<?xml version="1.0"?>
<feed xmlns="http://www.w3.org/2005/Atom" xml:lang="en">
	<id>http://earthwise.bgs.ac.uk/api.php?action=feedcontributions&amp;feedformat=atom&amp;user=Beod</id>
	<title>MediaWiki - User contributions [en]</title>
	<link rel="self" type="application/atom+xml" href="http://earthwise.bgs.ac.uk/api.php?action=feedcontributions&amp;feedformat=atom&amp;user=Beod"/>
	<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php/Special:Contributions/Beod"/>
	<updated>2026-05-27T17:45:57Z</updated>
	<subtitle>User contributions</subtitle>
	<generator>MediaWiki 1.42.3</generator>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Educational_Resources&amp;diff=58542</id>
		<title>Groundwater Educational Resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Educational_Resources&amp;diff=58542"/>
		<updated>2023-02-09T13:29:30Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Online training materials for water professionals */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Groundwater Training and Educational Resources&lt;br /&gt;
&lt;br /&gt;
   Please cite page as: Africa Groundwater Atlas. 2023. Groundwater Educational Resources. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
==Online training materials for water professionals==&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===&#039;&#039;Professional Drilling Management&#039;&#039; 2022 - Africa Groundwater Network (AGW-Net) and Ask for Water GmbH===&lt;br /&gt;
&lt;br /&gt;
This online training course on Professional Drilling Management was run in 2022, hosted on the [https://cap-net.org/ &#039;&#039;&#039;Cap-Net&#039;&#039;&#039;] UNDP virtual campus,  and managed by [https://ask-for-water.ch/ Ask for Water GmbH] and the [https://agw-net.org/ Africa Groundwater Network (AGW-Net)]. This, third, and revised edition of the course and accompanying manual was made possible thanks to generous financial contributions from the German [https://www.bgr.bund.de/EN/Home/homepage_node_en.html Federal Institute for Geosciences and Natural Resources] (BGR). Earlier versions of the course were developed and supported by many other institutions. &lt;br /&gt;
&lt;br /&gt;
A [https://rural-water-supply.net/en/resources/details/1090 &#039;&#039;&#039;report, training manual and key materials from this course&#039;&#039;&#039;] are available to download from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website. &lt;br /&gt;
&lt;br /&gt;
[[File:ProfDrilMan2022.jpg| 200px |centre| Professional Drilling Management training course 2022 ]]&lt;br /&gt;
&lt;br /&gt;
===&#039;&#039;Groundwater Resources Management&#039;&#039; 2022 - Africa Groundwater Network (AGW-NET) and Ask for Water GmbH===&lt;br /&gt;
&lt;br /&gt;
This online training course on Groundwater Resources Management was run in 2022, hosted on the [https://cap-net.org/ &#039;&#039;&#039;Cap-Net&#039;&#039;&#039;] UNDP virtual campus and managed by the [https://agw-net.org/ Africa Groundwater Network (AGW-Net)]  and [https://ask-for-water.ch/ Ask for Water GmbH]. This, first online edition of the course and the accompanying manual was made possible thanks to generous financial contributions from the German [https://www.bgr.bund.de/EN/Home/homepage_node_en.html Federal Institute for Geosciences and Natural Resources] (BGR). &lt;br /&gt;
&lt;br /&gt;
A [https://rural-water-supply.net/en/resources/details/1091 &#039;&#039;&#039;report, training manual and key materials from this course&#039;&#039;&#039;] are available to download from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website.&lt;br /&gt;
&lt;br /&gt;
In the past 10 years, several previous face-to-face 5-day short courses on Groundwater Management have been run in the regions of West, East and Southern Africa. They were implemented by AGW-Net, with the support of Cap-Net/UNDP along with partners like BGR, IAH/Burdon Network, Senegal River Basin Organisation (OMVS), SADC-GMI, Coordination Régionale des Usagers et Usagères du Bassin du Niger (CRU-BN), among others. Reports and training manuals from some of these courses are available from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website - see next section.&lt;br /&gt;
&lt;br /&gt;
[[File:GWResMan2022.JPG | 200px |centre| Groundwater Resources Management training course 2022 ]]&lt;br /&gt;
&lt;br /&gt;
===Rural Water Supply Network (RWSN) - various groundwater-related training courses===&lt;br /&gt;
&lt;br /&gt;
The [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) has supported many groundwater-related training courses for working professionals in the water sector, and makes many [https://rural-water-supply.net/en/resources/filter/214 training materials from these courses] available online. Many of these courses focussed on water borehole drilling, including managing the financial and logistical aspects of drilling projects, and technical aspects of borehole siting and drilling supervision. Others focussed on the basics of hydrogeology and groundwater theory. &lt;br /&gt;
&lt;br /&gt;
Please search the [https://rural-water-supply.net/en/resources/filter/214 &#039;&#039;&#039;RWSN collection&#039;&#039;&#039;] of resources for the full list of courses. &lt;br /&gt;
These are just a few examples:&lt;br /&gt;
&lt;br /&gt;
:- A short course on [https://rural-water-supply.net/fr/ressources/details/555 &#039;&#039;&#039;Basic Hydrogeology and Borehole Siting&#039;&#039;&#039;], held in Sierra Leone in 2013&lt;br /&gt;
:- A five-day course on [https://rural-water-supply.net/en/resources/details/897 &#039;&#039;&#039;Drilling Supervision&#039;&#039;&#039;], held with SADC-GMI in South Africa in 2018&lt;br /&gt;
:- A five-day course on [https://rural-water-supply.net/fr/ressources/details/756 &#039;&#039;&#039;Procurement, Costing &amp;amp; Pricing and Contract Management of Borehole Construction&#039;&#039;&#039;], held in Zambia in 2016&lt;br /&gt;
&lt;br /&gt;
[[File:TrainingCourseProfessionalisingBoreholes.jpg| 200px |centre| Procurement, Costing &amp;amp; Pricing and Contract Management of Borehole Construction ]]&lt;br /&gt;
&lt;br /&gt;
===Africa Groundwater Network (AGW-Net) - training course on &#039;&#039;Groundwater in Transboundary Basins&#039;&#039;, 2014===&lt;br /&gt;
&lt;br /&gt;
In 2014, the [https://agw-net.org/ Africa Groundwater Network] (AGW-Net) ran a series of training courses for Transboundary Basin Organisations across Africa, focusing on the Integration of Groundwater Management. The detailed [https://agw-net.org/courses/ &#039;&#039;&#039;training manuals&#039;&#039;&#039;] for these courses are freely available to download, in French and in English. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:AGW-NET-TrainingManualCover.JPG| 200px|thumb| left| [https://agw-net.org/wp-content/uploads/2020/04/GW-integration-into-River-Basin_Training_Manual_total_EN.pdf Training Manual] ]] &lt;br /&gt;
&lt;br /&gt;
[[File:AGW-NET-TrainingManualCover-FR.JPG| 200px|thumb| right| [https://agw-net.org/wp-content/uploads/2020/04/Integration-Eaux-Souterraine-Bassin-Transfrontalier_Training_Manual_total_FR.pdf Manuel de Formation] ]] &lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
==Educational resources for non-hydrogeologists==&lt;br /&gt;
&lt;br /&gt;
Here are some links to information and resources that can help explain groundwater issues and hydrogeology to non-hydrogeologists, including posters, fliers and other documents. Some of these are of general use worldwide and others are specifically relevant to an African context. They &lt;br /&gt;
&lt;br /&gt;
===[https://upgro.org/ UPGro]===&lt;br /&gt;
&lt;br /&gt;
The [https://upgro.org/ UPGro] research programme has produced a series of educational resources. These include:&lt;br /&gt;
&lt;br /&gt;
====[https://upgro.org/about/upgro-posters/  Groundwater Posters]====&lt;br /&gt;
&lt;br /&gt;
These [https://upgro.org/about/upgro-posters/ &#039;&#039;&#039;groundwater posters&#039;&#039;&#039;] carry important but simple messages about groundwater in Africa. They are available in English and French and are freely available to download as pdf posters.&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:2-groundwater-in-africa-poster-3.png| 200px|thumb| left| Groundwater in Africa - poster by UPGro]] &lt;br /&gt;
&lt;br /&gt;
[[File:poster_2_final_french-3.png| 200px|thumb| right| L&#039;eau souterraine en Afrique - affiche par UPGro]] &lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
====[https://upgro.org/consortium/gro-for-good/ Gro for GooD]==== &lt;br /&gt;
&lt;br /&gt;
The UPGro [https://upgro.org/consortium/gro-for-good/ &#039;&#039;&#039;Gro for GooD&#039;&#039;&#039;] project has produced an educational resource for  use by Kenyan secondary school students, called [https://upgro.files.wordpress.com/2018/03/water-module-student-resource-web.pdf &#039;&#039;&#039;The Water Module&#039;&#039;&#039;]. The Water Module was developed out of a programme of engagement to teach young people in Kwale County about water science and management. This [https://upgro.org/2018/03/22/back-to-school-the-future-of-water-starts-here-wwf8-worldwaterday2018/ &#039;&#039;&#039;blog post&#039;&#039;&#039;] gives a summary of this Schools Water Clubs programme and the Water Module student resource.&lt;br /&gt;
&lt;br /&gt;
[[File:TheWaterModuleFrontPage.PNG| 300px|center|thumb| The Water Module by Gro for Good]]&lt;br /&gt;
&lt;br /&gt;
===[https://iah.org/ IAH]===&lt;br /&gt;
&lt;br /&gt;
The International Association of Hydrogeologists ([https://iah.org/ IAH]) has a series of [https://iah.org/education &#039;&#039;&#039;educational resources&#039;&#039;&#039;] about groundwater and the science of hydrogeology. These include information for the [https://iah.org/education/general-public general public] and for [https://iah.org/education/professionals hydrogeology  students and professionals]. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[File:earthswatergraphic.png| 300px| centre| The Earth&#039;s water]] &lt;br /&gt;
 &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Educational_Resources&amp;diff=58541</id>
		<title>Groundwater Educational Resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Educational_Resources&amp;diff=58541"/>
		<updated>2023-02-09T13:28:09Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Groundwater Training and Educational Resources&lt;br /&gt;
&lt;br /&gt;
   Please cite page as: Africa Groundwater Atlas. 2023. Groundwater Educational Resources. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
==Online training materials for water professionals==&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Africa Groundwater Network (AGW-Net) and Ask for Water GmbH - training course on &#039;&#039;Professional Drilling Management&#039;&#039;, 2022===&lt;br /&gt;
&lt;br /&gt;
This online training course on Professional Drilling Management was run in 2022, hosted on the [https://cap-net.org/ &#039;&#039;&#039;Cap-Net&#039;&#039;&#039;] UNDP virtual campus,  and managed by [https://ask-for-water.ch/ Ask for Water GmbH] and the [https://agw-net.org/ Africa Groundwater Network (AGW-Net)]. This, third, and revised edition of the course and accompanying manual was made possible thanks to generous financial contributions from the German [https://www.bgr.bund.de/EN/Home/homepage_node_en.html Federal Institute for Geosciences and Natural Resources] (BGR). Earlier versions of the course were developed and supported by many other institutions. &lt;br /&gt;
&lt;br /&gt;
A [https://rural-water-supply.net/en/resources/details/1090 &#039;&#039;&#039;report, training manual and key materials from this course&#039;&#039;&#039;] are available to download from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website. &lt;br /&gt;
&lt;br /&gt;
[[File:ProfDrilMan2022.jpg| 200px |centre| Professional Drilling Management training course 2022 ]]&lt;br /&gt;
&lt;br /&gt;
===Africa Groundwater Network (AGW-NET) and Ask for Water GmbH - training course on &#039;&#039;Groundwater Resources Management&#039;&#039;, 2022===&lt;br /&gt;
&lt;br /&gt;
This online training course on Groundwater Resources Management was run in 2022, hosted on the [https://cap-net.org/ &#039;&#039;&#039;Cap-Net&#039;&#039;&#039;] UNDP virtual campus and managed by the [https://agw-net.org/ Africa Groundwater Network (AGW-Net)]  and [https://ask-for-water.ch/ Ask for Water GmbH]. This, first online edition of the course and the accompanying manual was made possible thanks to generous financial contributions from the German [https://www.bgr.bund.de/EN/Home/homepage_node_en.html Federal Institute for Geosciences and Natural Resources] (BGR). &lt;br /&gt;
&lt;br /&gt;
A [https://rural-water-supply.net/en/resources/details/1091 &#039;&#039;&#039;report, training manual and key materials from this course&#039;&#039;&#039;] are available to download from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website.&lt;br /&gt;
&lt;br /&gt;
In the past 10 years, several previous face-to-face 5-day short courses on Groundwater Management have been run in the regions of West, East and Southern Africa. They were implemented by AGW-Net, with the support of Cap-Net/UNDP along with partners like BGR, IAH/Burdon Network, Senegal River Basin Organisation (OMVS), SADC-GMI, Coordination Régionale des Usagers et Usagères du Bassin du Niger (CRU-BN), among others. Reports and training manuals from some of these courses are available from the [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) website - see next section.&lt;br /&gt;
&lt;br /&gt;
[[File:GWResMan2022.JPG | 200px |centre| Groundwater Resources Management training course 2022 ]]&lt;br /&gt;
&lt;br /&gt;
===Rural Water Supply Network (RWSN) - various groundwater-related training courses===&lt;br /&gt;
&lt;br /&gt;
The [https://rural-water-supply.net/en/ Rural Water Supply Network] (RWSN) has supported many groundwater-related training courses for working professionals in the water sector, and makes many [https://rural-water-supply.net/en/resources/filter/214 training materials from these courses] available online. Many of these courses focussed on water borehole drilling, including managing the financial and logistical aspects of drilling projects, and technical aspects of borehole siting and drilling supervision. Others focussed on the basics of hydrogeology and groundwater theory. &lt;br /&gt;
&lt;br /&gt;
Please search the [https://rural-water-supply.net/en/resources/filter/214 &#039;&#039;&#039;RWSN collection&#039;&#039;&#039;] of resources for the full list of courses. &lt;br /&gt;
These are just a few examples:&lt;br /&gt;
&lt;br /&gt;
:- A short course on [https://rural-water-supply.net/fr/ressources/details/555 &#039;&#039;&#039;Basic Hydrogeology and Borehole Siting&#039;&#039;&#039;], held in Sierra Leone in 2013&lt;br /&gt;
:- A five-day course on [https://rural-water-supply.net/en/resources/details/897 &#039;&#039;&#039;Drilling Supervision&#039;&#039;&#039;], held with SADC-GMI in South Africa in 2018&lt;br /&gt;
:- A five-day course on [https://rural-water-supply.net/fr/ressources/details/756 &#039;&#039;&#039;Procurement, Costing &amp;amp; Pricing and Contract Management of Borehole Construction&#039;&#039;&#039;], held in Zambia in 2016&lt;br /&gt;
&lt;br /&gt;
[[File:TrainingCourseProfessionalisingBoreholes.jpg| 200px |centre| Procurement, Costing &amp;amp; Pricing and Contract Management of Borehole Construction ]]&lt;br /&gt;
&lt;br /&gt;
===Africa Groundwater Network (AGW-Net) - training course on &#039;&#039;Groundwater in Transboundary Basins&#039;&#039;, 2014===&lt;br /&gt;
&lt;br /&gt;
In 2014, the [https://agw-net.org/ Africa Groundwater Network] (AGW-Net) ran a series of training courses for Transboundary Basin Organisations across Africa, focusing on the Integration of Groundwater Management. The detailed [https://agw-net.org/courses/ &#039;&#039;&#039;training manuals&#039;&#039;&#039;] for these courses are freely available to download, in French and in English. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:AGW-NET-TrainingManualCover.JPG| 200px|thumb| left| [https://agw-net.org/wp-content/uploads/2020/04/GW-integration-into-River-Basin_Training_Manual_total_EN.pdf Training Manual] ]] &lt;br /&gt;
&lt;br /&gt;
[[File:AGW-NET-TrainingManualCover-FR.JPG| 200px|thumb| right| [https://agw-net.org/wp-content/uploads/2020/04/Integration-Eaux-Souterraine-Bassin-Transfrontalier_Training_Manual_total_FR.pdf Manuel de Formation] ]] &lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
==Educational resources for non-hydrogeologists==&lt;br /&gt;
&lt;br /&gt;
Here are some links to information and resources that can help explain groundwater issues and hydrogeology to non-hydrogeologists, including posters, fliers and other documents. Some of these are of general use worldwide and others are specifically relevant to an African context. They &lt;br /&gt;
&lt;br /&gt;
===[https://upgro.org/ UPGro]===&lt;br /&gt;
&lt;br /&gt;
The [https://upgro.org/ UPGro] research programme has produced a series of educational resources. These include:&lt;br /&gt;
&lt;br /&gt;
====[https://upgro.org/about/upgro-posters/  Groundwater Posters]====&lt;br /&gt;
&lt;br /&gt;
These [https://upgro.org/about/upgro-posters/ &#039;&#039;&#039;groundwater posters&#039;&#039;&#039;] carry important but simple messages about groundwater in Africa. They are available in English and French and are freely available to download as pdf posters.&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:2-groundwater-in-africa-poster-3.png| 200px|thumb| left| Groundwater in Africa - poster by UPGro]] &lt;br /&gt;
&lt;br /&gt;
[[File:poster_2_final_french-3.png| 200px|thumb| right| L&#039;eau souterraine en Afrique - affiche par UPGro]] &lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
====[https://upgro.org/consortium/gro-for-good/ Gro for GooD]==== &lt;br /&gt;
&lt;br /&gt;
The UPGro [https://upgro.org/consortium/gro-for-good/ &#039;&#039;&#039;Gro for GooD&#039;&#039;&#039;] project has produced an educational resource for  use by Kenyan secondary school students, called [https://upgro.files.wordpress.com/2018/03/water-module-student-resource-web.pdf &#039;&#039;&#039;The Water Module&#039;&#039;&#039;]. The Water Module was developed out of a programme of engagement to teach young people in Kwale County about water science and management. This [https://upgro.org/2018/03/22/back-to-school-the-future-of-water-starts-here-wwf8-worldwaterday2018/ &#039;&#039;&#039;blog post&#039;&#039;&#039;] gives a summary of this Schools Water Clubs programme and the Water Module student resource.&lt;br /&gt;
&lt;br /&gt;
[[File:TheWaterModuleFrontPage.PNG| 300px|center|thumb| The Water Module by Gro for Good]]&lt;br /&gt;
&lt;br /&gt;
===[https://iah.org/ IAH]===&lt;br /&gt;
&lt;br /&gt;
The International Association of Hydrogeologists ([https://iah.org/ IAH]) has a series of [https://iah.org/education &#039;&#039;&#039;educational resources&#039;&#039;&#039;] about groundwater and the science of hydrogeology. These include information for the [https://iah.org/education/general-public general public] and for [https://iah.org/education/professionals hydrogeology  students and professionals]. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[File:earthswatergraphic.png| 300px| centre| The Earth&#039;s water]] &lt;br /&gt;
 &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58532</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58532"/>
		<updated>2023-01-31T16:07:21Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Artificial Recharge */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (artificial recharge), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. rainfall flows first over the land surface and into rivers or lakes before infiltrating down into aquifers in a different place from where it originally fell. Recharge can be diffuse, where water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, sometimes over large areas; or it can be focussed, where water infiltrates the ground preferentially at point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Recharge estimations for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable assessments of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers. There have been many site-specific studies of groundwater recharge at locations across Africa. These vary a lot in what estimation methods were used; in study scale; in the geographical, climatic and geological characteristics of the study region; and in the quality of data available. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except at coarse resolution as part of large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
A recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Controls on recharge in Africa===&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.jhydrol.2022.127967 &#039;&#039;&#039;West et al. (2022)&#039;&#039;&#039;] carried out a review of previous recharge studies across Africa to identify the dominant controls on recharge processes and volumes. They identified a number of climatic, topographic, vegetation, soil and geologic properties that appear to have consistent impacts on recharge, and developed a series of indices based on selected these properties to characterise different controls on recharge. They used these indices to divide Africa into 15 &#039;&#039;Recharge Landscape Units&#039;&#039; within which they suggest that recharge controls are likely to be similar. Over 80% of Africa&#039;s land area is accounted for by just nine of these units.&lt;br /&gt;
 &lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
[https://www.usgs.gov/mission-areas/water-resources/science/artificial-groundwater-recharge &#039;&#039;Artificial recharge&#039;&#039;] is the human, planned activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are &#039;&#039;Managed Aquifer Recharge&#039;&#039; and &#039;&#039;Aquifer Storage and Recovery&#039;&#039;. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]. Includes a number of specific studies in Africa, including an online viewer of [https://ggis.un-igrac.org/layers/mar_global:mar_global:marpotential_south_africa &#039;&#039;&#039;map of potential artificial recharge areas in South Africa&#039;&#039;&#039;], produced by the South African Department of Water Affairs (2009)&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.artificialrecharge.co.za/ &#039;&#039;&#039;South Africa&#039;s Artificial Recharge Information Centre&#039;&#039;&#039;]. This site contains information particularly relevant to South African conditions on Artificial Recharge (AR), Managed Aquifer Recharge (MAR) and Aquifer Storage and Recovery (ASR). &lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augmentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2022. [https://doi.org/10.1016/j.jhydrol.2022.127967 Understanding process controls on groundwater recharge variability across Africa through recharge landscapes]. Journal of Hydrology 612, Part A.&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58531</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58531"/>
		<updated>2023-01-31T16:07:12Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Artificial Recharge */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (artificial recharge), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. rainfall flows first over the land surface and into rivers or lakes before infiltrating down into aquifers in a different place from where it originally fell. Recharge can be diffuse, where water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, sometimes over large areas; or it can be focussed, where water infiltrates the ground preferentially at point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Recharge estimations for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable assessments of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers. There have been many site-specific studies of groundwater recharge at locations across Africa. These vary a lot in what estimation methods were used; in study scale; in the geographical, climatic and geological characteristics of the study region; and in the quality of data available. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except at coarse resolution as part of large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
A recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Controls on recharge in Africa===&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.jhydrol.2022.127967 &#039;&#039;&#039;West et al. (2022)&#039;&#039;&#039;] carried out a review of previous recharge studies across Africa to identify the dominant controls on recharge processes and volumes. They identified a number of climatic, topographic, vegetation, soil and geologic properties that appear to have consistent impacts on recharge, and developed a series of indices based on selected these properties to characterise different controls on recharge. They used these indices to divide Africa into 15 &#039;&#039;Recharge Landscape Units&#039;&#039; within which they suggest that recharge controls are likely to be similar. Over 80% of Africa&#039;s land area is accounted for by just nine of these units.&lt;br /&gt;
 &lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
[https://www.usgs.gov/mission-areas/water-resources/science/artificial-groundwater-recharge &#039;&#039;Artificial recharge&#039;&#039;] is the human, planned activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are &#039;&#039;Managed Aquifer Recharge&#039;&#039; and &#039;&#039;Aquifer Storage and Recovery&#039;&#039;. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]. Includes a number of specific studies in Africa, including an online viewer of [https://ggis.un-igrac.org/layers/mar_global:mar_global:marpotential_south_africa &#039;&#039;&#039;map of potential artificial recharge areas in South Africa&#039;&#039;&#039;], produced by the South African Department of Water Affairs (2009)&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.artificialrecharge.co.za/ &#039;&#039;&#039;South Africa&#039;s Artificial Recharge Information Centre&#039;&#039;&#039;]. This site contains information particularly relevant to South African conditions on Artificial Recharge (AR), Managed Aquifer Recharge (MAR) and Aquifer Storage and Recovery (ASR). &lt;br /&gt;
&lt;br /&gt;
:- &lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augmentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2022. [https://doi.org/10.1016/j.jhydrol.2022.127967 Understanding process controls on groundwater recharge variability across Africa through recharge landscapes]. Journal of Hydrology 612, Part A.&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58530</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58530"/>
		<updated>2023-01-31T15:50:27Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (artificial recharge), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. rainfall flows first over the land surface and into rivers or lakes before infiltrating down into aquifers in a different place from where it originally fell. Recharge can be diffuse, where water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, sometimes over large areas; or it can be focussed, where water infiltrates the ground preferentially at point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Recharge estimations for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable assessments of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers. There have been many site-specific studies of groundwater recharge at locations across Africa. These vary a lot in what estimation methods were used; in study scale; in the geographical, climatic and geological characteristics of the study region; and in the quality of data available. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except at coarse resolution as part of large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
A recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Controls on recharge in Africa===&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.jhydrol.2022.127967 &#039;&#039;&#039;West et al. (2022)&#039;&#039;&#039;] carried out a review of previous recharge studies across Africa to identify the dominant controls on recharge processes and volumes. They identified a number of climatic, topographic, vegetation, soil and geologic properties that appear to have consistent impacts on recharge, and developed a series of indices based on selected these properties to characterise different controls on recharge. They used these indices to divide Africa into 15 &#039;&#039;Recharge Landscape Units&#039;&#039; within which they suggest that recharge controls are likely to be similar. Over 80% of Africa&#039;s land area is accounted for by just nine of these units.&lt;br /&gt;
 &lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2022. [https://doi.org/10.1016/j.jhydrol.2022.127967 Understanding process controls on groundwater recharge variability across Africa through recharge landscapes]. Journal of Hydrology 612, Part A.&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58529</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58529"/>
		<updated>2023-01-31T15:13:46Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Recharge estimations for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (i.e., &amp;quot;artificial groundwater recharge&amp;quot;), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. surface water flows first over impermeable land and into rivers or lakes before later infiltrating down into aquifers in a different place from where it fell as rain. It can be diffuse, e.g. water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, which can be distributed over large areas; or it can be focussed recharge, e.g. where water infiltrates from point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Recharge estimations for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58528</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58528"/>
		<updated>2023-01-31T15:13:13Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (i.e., &amp;quot;artificial groundwater recharge&amp;quot;), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. surface water flows first over impermeable land and into rivers or lakes before later infiltrating down into aquifers in a different place from where it fell as rain. It can be diffuse, e.g. water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, which can be distributed over large areas; or it can be focussed recharge, e.g. where water infiltrates from point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Recharge estimations for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are: chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers.&lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58527</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58527"/>
		<updated>2023-01-31T12:01:11Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (i.e., &amp;quot;artificial groundwater recharge&amp;quot;), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. surface water flows first over impermeable land and into rivers or lakes before later infiltrating down into aquifers in a different place from where it fell as rain. It can be diffuse, e.g. water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, which can be distributed over large areas; or it can be focussed recharge, e.g. where water infiltrates from point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. The most common methods to estimate recharge rates are: chloride mass balance; soil physics methods; environmental and isotopic tracers; groundwater level fluctuation methods; water balance methods (including numerical groundwater modelling) and the estimation of baseflow to rivers.&lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58526</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58526"/>
		<updated>2023-01-31T12:00:10Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* What is recharge? */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is (groundwater) recharge?==&lt;br /&gt;
&lt;br /&gt;
[https://en.wikipedia.org/wiki/Groundwater_recharge &#039;&#039;&#039;Groundwater recharge&#039;&#039;&#039;] - which hydrogeologists just call recharge - is a hydrological process which results in the replenishment, or renewal, of groundwater in aquifers. Recharge is the main control on the volume of renewable groundwater resource. &lt;br /&gt;
&lt;br /&gt;
Recharge processes are very variable, and controlled by many factors including climatic zone, weather patterns, geology and land use. Recharge can be natural (through the water cycle) and/or through anthropogenic processes (i.e., &amp;quot;artificial groundwater recharge&amp;quot;), where rainwater, surface water and/or reclaimed water is deliberately routed to aquifers. It can be direct - where rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - e.g. surface water flows first over impermeable land and into rivers or lakes before later infiltrating down into aquifers in a different place from where it fell as rain. It can be diffuse, e.g. water (rainwater or artificially applied water) infiltrates through the soil and any superficial deposits or bedrock to the water table, which can be distributed over large areas; or it can be focussed recharge, e.g. where water infiltrates from point sources or small areas, such as wadis or lakes, or land surface depressions.&lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58525</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58525"/>
		<updated>2023-01-30T15:02:44Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58524</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58524"/>
		<updated>2023-01-30T15:02:23Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. &lt;br /&gt;
&lt;br /&gt;
However, a recent study by [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] provided a more detailed recharge estimate for the whole of Africa. This has also been used to ground-truth recharge estimates for Africa from eight global scale models, by [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58523</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58523"/>
		<updated>2023-01-30T15:00:43Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. This was the first ground-based approximation of recharge across the whole of Africa. They estimate that average recharge every decade in Africa is 15 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt; (4900–45 000 km&amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;), or approximately 2% of estimated groundwater storage across the continent. However, recharge across Africa is characterised by great variability between different aquifer types (hydrogeological environments): in particular, between sedimentary aquifers in North Africa (high storage and low recharge) and weathered crystalline/basement rock aquifers (low storage and high recharge) across much of tropical Africa. &lt;br /&gt;
&lt;br /&gt;
The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58522</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58522"/>
		<updated>2023-01-30T14:56:19Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;] compare recharge and recharge ratio (annual recharge/annual precipitation) estimates from eight global models with the same dataset of over 100 ground-based estimates in Africa. They showed that global modelled recharge estimates disagree significantly across the different landscapes of Africa, and also vary considerably and inconsistently in how closely they match ground-based estimates. The global-scale models that allowed stronger climatic controls on their recharge estimates were more similar to ground-based estimates in Africa. The authors stress that this means groundwater recharge prediction across Africa should not rely on estimates from a single model but instead look at the distribution of estimates from different models.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58521</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58521"/>
		<updated>2023-01-30T14:50:50Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 &#039;&#039;&#039;UK government open data repository&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58520</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58520"/>
		<updated>2023-01-30T14:50:28Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
In their paper, [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on 134 ground-based estimates. The digital, georeferenced recharge map and a database of the ground-based recharge estimates are available to download from the [https://www.data.gov.uk/dataset/2542c410-e8ea-42c7-a33c-f78713a5a480/groundwater-recharge-in-africa-from-ground-based-measurements-nerc-grant-ne-l002035-1 UK government open data repository].&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58519</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58519"/>
		<updated>2023-01-30T14:39:40Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Hydrogeological_Processes_Africa&amp;diff=58518</id>
		<title>Hydrogeological Processes Africa</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Hydrogeological_Processes_Africa&amp;diff=58518"/>
		<updated>2023-01-30T14:39:20Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Key hydrogeological processes */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Key hydrogeological processes, with particular reference to Africa&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
==Key hydrogeological processes==&lt;br /&gt;
&lt;br /&gt;
These pages provide background on the hydrogeological processes that are an essential part of understanding groundwater resources and hydrogeology, and specific information relevant to Africa. &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge in Africa]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality in Africa]], including groundwater chemistry&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58517</id>
		<title>Additional resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58517"/>
		<updated>2023-01-30T14:38:58Z</updated>

		<summary type="html">&lt;p&gt;Beod: /*  Key hydrogeological processes */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Information resources on groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
These pages provide background information on many different aspects of groundwater and hydrogeology, with particular relevance to Africa, and links to more detailed resources. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Overview_of_Groundwater_in_Africa| An overview of groundwater in Africa]]===&lt;br /&gt;
&lt;br /&gt;
A brief [[Overview_of_Groundwater_in_Africa| background to groundwater resources and hydrogeological environments in Africa]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
These pages have information on the geological and other environmental maps and graphs on the country pages: how they were developed, and links to original data sources.&lt;br /&gt;
&lt;br /&gt;
:- [[Geography| Country boundaries and land surface elevation]]&lt;br /&gt;
&lt;br /&gt;
:- [[Geology  | Geology]]&lt;br /&gt;
&lt;br /&gt;
:- [[Climate | Climate]]&lt;br /&gt;
&lt;br /&gt;
:- [[Land cover | Land cover]]&lt;br /&gt;
&lt;br /&gt;
:- [[Soil | Soil]] &lt;br /&gt;
&lt;br /&gt;
:- [[Surface water | Surface water]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeological Processes Africa| Key hydrogeological processes]]===&lt;br /&gt;
&lt;br /&gt;
An overview of key hydrogeological processes, with particular relevance to Africa: &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge in Africa]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality in Africa]]&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology Maps Of Africa | Overview of groundwater and hydrogeological maps of Africa]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Hydrogeology Maps Of Africa | Groundwater and hydrogeological maps of Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa Groundwater Atlas Hydrogeology Maps | The Africa Groundwater Atlas country hydrogeology maps]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Developing groundwater resources | Developing groundwater resources]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater development techniques | Introduction to groundwater development procedures]]&lt;br /&gt;
&lt;br /&gt;
:- [[Borehole Drilling | Borehole Drilling]], including professionalising drilling&lt;br /&gt;
&lt;br /&gt;
:- [[Manual drilling | Manual drilling]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes | Siting Boreholes]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes:Reconnaissance | Siting Boreholes:Reconnaissance]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Groundwater Source Yield |Assessing source yield]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Water Quality | Assessing water quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Management | Groundwater management]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater management organisations | Groundwater management organisations]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater Data | Groundwater data]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater use | Groundwater use in Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Data | Groundwater data]]===&lt;br /&gt;
&lt;br /&gt;
Information on and links to sources of [[Groundwater Data | groundwater data]] in Africa.&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa National Groundwater Databases | &#039;&#039;&#039;Inventory of national groundwater databases in Africa&#039;&#039;&#039;]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Key Groundwater Issues | Key groundwater issues]]===&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
:-[[Urban groundwater in Africa | Urban groundwater in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater irrigation in Africa | Groundwater and irrigation in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Transboundary aquifers | Transboundary aquifers]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Case studies===&lt;br /&gt;
&lt;br /&gt;
:- A series of [[Case studies | &#039;&#039;&#039;case studies&#039;&#039;&#039;]] that illustrate different groundwater understanding and management issues across Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Research in Africa | Groundwater Research in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Information on key current and past groundwater research themes and projects in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Educational Resources | Groundwater Training and Educational Resources]]===&lt;br /&gt;
&lt;br /&gt;
Information and resources on online training courses and course material for water professionals, and educational resources to help explain groundwater issues and hydrogeology.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Organisations in Africa | Groundwater Organisations in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Links to some of the  many professional networks and organisations offer support to those working in groundwater and hydrogeology in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58516</id>
		<title>Additional resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58516"/>
		<updated>2023-01-30T14:38:41Z</updated>

		<summary type="html">&lt;p&gt;Beod: /*  Key hydrogeological processes */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Information resources on groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
These pages provide background information on many different aspects of groundwater and hydrogeology, with particular relevance to Africa, and links to more detailed resources. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Overview_of_Groundwater_in_Africa| An overview of groundwater in Africa]]===&lt;br /&gt;
&lt;br /&gt;
A brief [[Overview_of_Groundwater_in_Africa| background to groundwater resources and hydrogeological environments in Africa]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
These pages have information on the geological and other environmental maps and graphs on the country pages: how they were developed, and links to original data sources.&lt;br /&gt;
&lt;br /&gt;
:- [[Geography| Country boundaries and land surface elevation]]&lt;br /&gt;
&lt;br /&gt;
:- [[Geology  | Geology]]&lt;br /&gt;
&lt;br /&gt;
:- [[Climate | Climate]]&lt;br /&gt;
&lt;br /&gt;
:- [[Land cover | Land cover]]&lt;br /&gt;
&lt;br /&gt;
:- [[Soil | Soil]] &lt;br /&gt;
&lt;br /&gt;
:- [[Surface water | Surface water]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeological Processes Africa| Key hydrogeological processes]]===&lt;br /&gt;
&lt;br /&gt;
An overview of key hydrogeological processes, with particular relevance to Africa: &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge in Africa]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology Maps Of Africa | Overview of groundwater and hydrogeological maps of Africa]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Hydrogeology Maps Of Africa | Groundwater and hydrogeological maps of Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa Groundwater Atlas Hydrogeology Maps | The Africa Groundwater Atlas country hydrogeology maps]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Developing groundwater resources | Developing groundwater resources]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater development techniques | Introduction to groundwater development procedures]]&lt;br /&gt;
&lt;br /&gt;
:- [[Borehole Drilling | Borehole Drilling]], including professionalising drilling&lt;br /&gt;
&lt;br /&gt;
:- [[Manual drilling | Manual drilling]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes | Siting Boreholes]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes:Reconnaissance | Siting Boreholes:Reconnaissance]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Groundwater Source Yield |Assessing source yield]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Water Quality | Assessing water quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Management | Groundwater management]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater management organisations | Groundwater management organisations]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater Data | Groundwater data]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater use | Groundwater use in Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Data | Groundwater data]]===&lt;br /&gt;
&lt;br /&gt;
Information on and links to sources of [[Groundwater Data | groundwater data]] in Africa.&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa National Groundwater Databases | &#039;&#039;&#039;Inventory of national groundwater databases in Africa&#039;&#039;&#039;]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Key Groundwater Issues | Key groundwater issues]]===&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
:-[[Urban groundwater in Africa | Urban groundwater in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater irrigation in Africa | Groundwater and irrigation in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Transboundary aquifers | Transboundary aquifers]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Case studies===&lt;br /&gt;
&lt;br /&gt;
:- A series of [[Case studies | &#039;&#039;&#039;case studies&#039;&#039;&#039;]] that illustrate different groundwater understanding and management issues across Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Research in Africa | Groundwater Research in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Information on key current and past groundwater research themes and projects in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Educational Resources | Groundwater Training and Educational Resources]]===&lt;br /&gt;
&lt;br /&gt;
Information and resources on online training courses and course material for water professionals, and educational resources to help explain groundwater issues and hydrogeology.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Organisations in Africa | Groundwater Organisations in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Links to some of the  many professional networks and organisations offer support to those working in groundwater and hydrogeology in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58515</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58515"/>
		<updated>2023-01-30T14:37:42Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more content.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | &#039;&#039;&#039;a review of recharge estimation techniques used in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58514</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58514"/>
		<updated>2023-01-30T14:37:31Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more content.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [https://upgro.org/catalyst-projects/groundwater-recharge/  &#039;&#039;&#039;UPGro project&#039;&#039;&#039;] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | a review of recharge estimation techniques used in Africa]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58513</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58513"/>
		<updated>2023-01-30T14:37:15Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Estimating recharge for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more content.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [[https://upgro.org/catalyst-projects/groundwater-recharge/  UPGro project] in 2014, and is included in full on this page - [[#A review of recharge estimation techniques used in Africa | a review of recharge estimation techniques used in Africa]].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 &#039;&#039;&#039;Berghuijs et al. (2022)&#039;&#039;&#039;], [[https://doi.org/10.1016/j.scitotenv.2020.137042 &#039;&#039;&#039;Moeck et al. (2020)&#039;&#039;&#039;] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html &#039;&#039;&#039;Döll and Fiedler (2008)&#039;&#039;&#039;]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates.&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58512</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58512"/>
		<updated>2023-01-30T14:36:38Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
  This page is in the process of being updated. Please check back soon for more content.&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [[https://upgro.org/catalyst-projects/groundwater-recharge/  UPGro project] in 2014, and is included in full on this page - [#A review of recharge estimation techniques used in Africa | a review of recharge estimation techniques used in Africa].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 Berghuijs et al. (2022)], [[https://doi.org/10.1016/j.scitotenv.2020.137042 Moeck et al. (2020)] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Döll and Fiedler (2008)]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58511</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58511"/>
		<updated>2023-01-30T14:36:07Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge in Africa&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2023. Recharge in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [[https://upgro.org/catalyst-projects/groundwater-recharge/  UPGro project] in 2014, and is included in full on this page - [#A review of recharge estimation techniques used in Africa | a review of recharge estimation techniques used in Africa].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 Berghuijs et al. (2022)], [[https://doi.org/10.1016/j.scitotenv.2020.137042 Moeck et al. (2020)] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Döll and Fiedler (2008)]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58510</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58510"/>
		<updated>2023-01-30T14:35:40Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing. &lt;br /&gt;
&lt;br /&gt;
There have been many site-specific studies of groundwater recharge at locations across Africa. These vary significantly in the study scale; the geographical, climatic and geological characteristics of the study region; the quality of data available; and the estimation methods used. A detailed review of recharge estimation techniques used in more than 200 studies across Africa was written by global experts in recharge, WM Edmunds and BR Scanlon, for an [[https://upgro.org/catalyst-projects/groundwater-recharge/  UPGro project] in 2014, and is included in full on this page - [#A review of recharge estimation techniques used in Africa | a review of recharge estimation techniques used in Africa].&lt;br /&gt;
&lt;br /&gt;
Until recently, recharge rates had not been mapped across the whole of Africa, except from large scale global models, such as [https://doi.org/10.1029/2022GL099010 Berghuijs et al. (2022)], [[https://doi.org/10.1016/j.scitotenv.2020.137042 Moeck et al. (2020)] and [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Döll and Fiedler (2008)]. Two recent studies have provided more detailed recharge estimates for the African continent: [https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] and [https://doi.org/10.1016/j.scitotenv.2022.159765 &#039;&#039;&#039;West et al. (2023)&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
[https://dx.doi.org/10.1088/1748-9326/abd661 &#039;&#039;&#039;MacDonald et al. (2021)&#039;&#039;&#039;] quantify long-term average distributed groundwater recharge rates across Africa based on over 100 ground-based estimates. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Berghuijs WR, Luijendijk E, Moeck C, Van der Velde Y and Allen S. 2022. [https://doi.org/10.1029/2022GL099010 Global Recharge Data Set Indicates Strengthened Groundwater Connection to Surface Fluxes]. Geophysical Research Letters 49. Doi:10.1029/2022GL099010. &lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Döll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Moeck C, Grech-Cumbo N, Podgorski J, Bretzler A, Gurdak JJ, Berg M, Schirmer M. 2020. [https://doi.org/10.1016/j.scitotenv.2020.137042 A global-scale dataset of direct natural groundwater recharge rates: A review of variables, processes and relationships]. Science of the Total Environment 15. Doi: 10.1016/j.scitotenv.2020.137042&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
West C, Reinecke R, Rosolem R, MacDonald AM, Cuthbert MO and Wagener T. 2023. [https://doi.org/10.1016/j.scitotenv.2022.159765 Ground truthing global-scale model estimates of groundwater recharge across Africa]. Science of The Total Environment 858 (3). Doi: 10.1016/j.scitotenv.2022.159765 . &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58509</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58509"/>
		<updated>2023-01-30T13:59:29Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* References */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
There have been many studies of groundwater recharge across Africa. These vary significantly in terms of the study scale; the geographical, climatic and geological characteristics of the region of interest; the quality of data used; and the estimation methods applied. This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
==Global recharge estimates==&lt;br /&gt;
&lt;br /&gt;
At a global scale, Döll and Fiedler (2008) provide estimates of long term average diffuse groundwater recharge based on the WaterGAP Global Hydrology Model. The model is run with a daily time-step at a spatial resolution of 0.5°, and is driven by gridded precipitation data. Model parameters are adjusted to match observed long-term average river discharge at more than 1000 gauging stations around the world. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Doll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security]. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58508</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58508"/>
		<updated>2023-01-30T13:59:16Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* References */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
There have been many studies of groundwater recharge across Africa. These vary significantly in terms of the study scale; the geographical, climatic and geological characteristics of the region of interest; the quality of data used; and the estimation methods applied. This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
==Global recharge estimates==&lt;br /&gt;
&lt;br /&gt;
At a global scale, Döll and Fiedler (2008) provide estimates of long term average diffuse groundwater recharge based on the WaterGAP Global Hydrology Model. The model is run with a daily time-step at a spatial resolution of 0.5°, and is driven by gridded precipitation data. Model parameters are adjusted to match observed long-term average river discharge at more than 1000 gauging stations around the world. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Doll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
MacDonald AM et al. 2021. [https://dx.doi.org/10.1088/1748-9326/abd661 Mapping groundwater recharge in Africa from ground observations and implications for water security. Environmental Research Letters 16 (3). Doi:10.1088/1748-9326/abd661&lt;br /&gt;
&lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58507</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58507"/>
		<updated>2023-01-30T13:57:00Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* A review of recharge estimation techniques for Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques used in Africa==&lt;br /&gt;
&lt;br /&gt;
There have been many studies of groundwater recharge across Africa. These vary significantly in terms of the study scale; the geographical, climatic and geological characteristics of the region of interest; the quality of data used; and the estimation methods applied. This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
==Global recharge estimates==&lt;br /&gt;
&lt;br /&gt;
At a global scale, Döll and Fiedler (2008) provide estimates of long term average diffuse groundwater recharge based on the WaterGAP Global Hydrology Model. The model is run with a daily time-step at a spatial resolution of 0.5°, and is driven by gridded precipitation data. Model parameters are adjusted to match observed long-term average river discharge at more than 1000 gauging stations around the world. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Doll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58506</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58506"/>
		<updated>2023-01-30T13:56:46Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Estimating recharge==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure when assessing groundwater resources, but in order to make reliable estimates of sustainable groundwater resources, it is vital to know how much recharge is occurring to aquifers, and extremely useful to understand recharge processes and timing.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==A review of recharge estimation techniques for Africa==&lt;br /&gt;
&lt;br /&gt;
There have been many studies of groundwater recharge across Africa. These vary significantly in terms of the study scale; the geographical, climatic and geological characteristics of the region of interest; the quality of data used; and the estimation methods applied. This review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. This project assessed more than 200 individual recharge studies carried out across Africa, and investigated what these studies can tell us about relationships between rainfall and recharge, and evidence for the thresholds controlling recharge, in Africa. The review authors were [https://nora.nerc.ac.uk/id/eprint/519410/1/Professor%20Wyndham%20Michael%20Edmunds%20Final.pdf &#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;], formerly of the University of Oxford, UK; and [https://www.jsg.utexas.edu/researcher/bridget_scanlon/ &#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;], of the University of Texas, USA.&lt;br /&gt;
&lt;br /&gt;
Key findings of the review were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- there are broad relationships between average rainfall and recharge, but these relationships become nonlinear when long term rainfall is very low - less than 500 mm average annual rainfall. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
==Global recharge estimates==&lt;br /&gt;
&lt;br /&gt;
At a global scale, Döll and Fiedler (2008) provide estimates of long term average diffuse groundwater recharge based on the WaterGAP Global Hydrology Model. The model is run with a daily time-step at a spatial resolution of 0.5°, and is driven by gridded precipitation data. Model parameters are adjusted to match observed long-term average river discharge at more than 1000 gauging stations around the world. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Doll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58505</id>
		<title>Recharge</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Recharge&amp;diff=58505"/>
		<updated>2023-01-30T13:50:01Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Recharge. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is recharge?==&lt;br /&gt;
Recharge is the replenishment of groundwater in aquifers by rainfall. Recharge can be direct - rainfall infiltrates directly into aquifers through soil, sediments or rock; or it can be indirect - surface water flows first over impermeable land and into rivers before later infiltrating down into aquifers in a different place from where it fell as rain. Recharge is one of the main controls on groundwater resources. &lt;br /&gt;
&lt;br /&gt;
==Recharge estimation techniques for Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater recharge is one of the most difficult parameters to measure in the assessment of groundwater resources, but it is vital for reliable projections of sustainable resource development.&lt;br /&gt;
&lt;br /&gt;
There have been many studies of groundwater recharge across Africa. These vary significantly in terms of the study scale; the geographical, climatic and geological characteristics of the region of interest; the quality of data used; and the estimation methods applied. The following review was written for the UPGro project [https://upgro.org/catalyst-projects/groundwater-recharge/ Groundwater recharge in Africa: identifying critical thresholds], which finished in 2014. The project reviewed more than 200 recharge studies in Africa, examining relationships between rainfall and recharge, and evidence for thresholds controlling recharge. Key findings were:&lt;br /&gt;
&lt;br /&gt;
- the importance of using multiple methods to estimate recharge&lt;br /&gt;
&lt;br /&gt;
- the importance of reporting recharge as decadal, rather than annual averages, because of the high year-to-year variability in recharge, particularly in semi-arid and arid regions&lt;br /&gt;
&lt;br /&gt;
- while broad relationships exist between average rainfall and recharge, such relationships become nonlinear when long-term average annual rainfall is less than 500 mm. Rainfall intensity and land cover are also important controls on recharge. In future, climate change is expected to lead to increased rainfall intensity, and so a better understanding of the role of episodic high intensity rainfall events in governing recharge will become increasingly important.&lt;br /&gt;
&lt;br /&gt;
===Authors===&lt;br /&gt;
&lt;br /&gt;
&#039;&#039;&#039;W M Edmunds&#039;&#039;&#039;, formerly University of Oxford, UK&lt;br /&gt;
&lt;br /&gt;
&#039;&#039;&#039;B R Scanlon&#039;&#039;&#039;, University of Texas, USA&lt;br /&gt;
&lt;br /&gt;
===Introduction===&lt;br /&gt;
&lt;br /&gt;
The major limiting factor in the sustainable use and management of Africa’s water resources is whether the stored groundwater is renewable or non-renewable.  Numerous studies have shown that in arid and many semi-arid areas the large bodies of fresh and useable groundwater reserves are non-renewable i.e. palaeowater recharged under wetter climates of the early Holocene or late Pleistocene, prior to the onset of a more arid climate around 4500 years BP (Edmunds et al., 2004). &lt;br /&gt;
&lt;br /&gt;
The purpose of this review is to examine the methods for estimating active, renewable recharge in the African context according the contrasting geology and hydrogeological contexts as well as the range in present-day hydroclimatic conditions. Techniques for characterising the non-renewable components are well documented. This review will focus on low-rainfall areas which depend critically on the renewable shallow groundwater. Many higher-rainfall areas also depend on groundwater for a safe source of water but the quantities are mostly reliable except in areas with seasonal (monsoonal) rains during prolonged dry seasons. A range of techniques are available which attempt to quantify modern recharge and rates can vary widely according to rock type and landscape. Several useful reviews are available, some of which are relevant to Africa (Simmers et al., 1988; Scanlon, Healy and Cook, 2002; Xu and Beekman, 2003; Scanlon et al., 2006). This review is selective and focuses on those methods which are most widely used, likely to have wide and practical application, and can be applied or adapted to local rather than regional scales over the African continent.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig1.png| 500px | center| thumb| Main landscape elements and recharge environments of northern Africa typified by a section from Central Sahara to the Guinea]]&lt;br /&gt;
&lt;br /&gt;
The geology of Africa presents several types of terrain that can be considered as major units for groundwater recharge. Several large sedimentary basins store groundwater predominantly as palaeowater, especially in North Africa (Sahara/Sahel) but also in southern Africa and in its coastal margins. In many of these areas the water table is deep and modern replenishment not an issue, but in basin margins the shallow water tables may receive modern recharge. Most sedimentary aquifers contain clastic sediments (limestones are rare except coastal margins); where sandstones dominate, recharge may be significant even with moderate or low rainfall. Secondly, large areas of Africa are covered by permeable sands of Quaternary age; these deposits, e.g. dune fields from former arid climates, may extend into wetter areas such as the Gulf areas of West Africa. Volcanic rocks, found mainly in the East African rift valley, have significant resources of renewable groundwater. Large areas of ancient igneous and metamorphic rocks form the basement and these rocks, traditionally considered as low permeability, are likely to give rise to the most important aquifer series per capita. The likelihood of modern recharge to groundwater in basement fracture systems and the regolith is a main challenge and topic of this review.&lt;br /&gt;
&lt;br /&gt;
===The interface between modern water and palaeowater===&lt;br /&gt;
&lt;br /&gt;
Geology and climate create constraints on groundwater recharge. Controls on both diffuse rainfall recharge and to focused recharge via wadis or depressions need to be considered, which may be influenced by terrain (slope) as well as soils and bedrock geology. Vegetation cover and its variation with time is an important variable, and the impact of rapid land-use change (e.g. clearance of trees and scrub) may increase recharge rates considerably. It is also possible that, if salinity in dryland areas increases as a result of changes in vegetation, this can cause water stored for millennia in the unsaturated zone to infiltrate down to the water table (Allison et al.1990).&lt;br /&gt;
It is very important therefore that recharge assessment is based in advance upon a reconnaissance of the best available knowledge of landscape, geological and environmental evidence. &lt;br /&gt;
&lt;br /&gt;
Shallow groundwater (&amp;lt;30 m) is most valuable for rural development and most productive wells are to be found within this limit in both hard and soft rock terrain. Construction by manual work or mobile drilling rigs is straightforward within this 30 m range. Where communities rely on such wells at the present day this may be a first sign that renewable groundwater exists. Across much of the semi-arid regions of Africa the balance between renewable and non-resources is critical. Chemical and isotopic tracer studies have been shown as the best way to demonstrate their presence especially in the widely distributed clastic sedimentary aquifers. The case study from Abu Delaig Sudan (see inset) indicates that zero diffuse recharge takes place through the unsaturated zone, yet focused recharge from wadis is an important renewable resource and that palaeowaters at depth are non-renewable under present-day climates. This emphasises the need to understand the relationships between water movement in both the unsaturated and saturated zones.&lt;br /&gt;
&lt;br /&gt;
The regolith presents many challenges for recharge and resource estimation.[should we include a modified Acworth diagram?]. It is characteristically heterogeneous with layering and/or lenses of permeable sandy material and interbedded clays, typically overlying permeable material overlying the basement rock; the depth to the latter (0 to 30 m typical) is variable depending on many geological factors (not discussed here). Surface deposits are frequently sandy and permeable but recharge may be hindered by clay lenses. Drilling may also intercept groundwater lenses which are not in hydraulic continuity with the main aquifer.&lt;br /&gt;
&lt;br /&gt;
{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ Case study of Abu Delaig and the Nile Valley&lt;br /&gt;
|Wadi Hawad with its minor tributaries lies in the Butana region of Sudan between the Nile and the Atbara Rivers, underlain by an embayment of the Nubian Sandstone Series (Cretaceous) which in turn overlies the Basement complex. The interfluve areas are flat grassland with sandy soil but often with a clay matrix which imparts a relatively impermeable surface. Much of the area is grazed by local or nomadic farmers who rely not only on the shallow groundwater resource exploited by hand dug wells (to 26 m) but also on several deep (to 150 m) pumped boreholes drilled in the Nubian sandstone.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1.png | 400 px |thumb|  left | Schematic cross section of Wadi Hawad showing groundwater recharge and likely water resources]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File: RC-BoxFig1b.png | 400px| thumb| right |Schematic cross section near town of Abu Delaig, with negligible direct recharge via the predominantly clay surface of the interfluve, as shown by chloride profiles. Recharge through wadi beds extends laterally beneath interfluves, as indicated by tritium. It is uncertain to what extent water from these &#039;freshwater lenses&#039; recharges the deeper aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
[[File: RC-BoxFig.png| 400px | center | thumb|Summary diagram of all isotopic data from the Wadi Hawai area - rainwater; River Nile; and shallow &amp;amp; deep groundwater, including moisture in the unsaturated zone]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Measuring groundwater recharge===&lt;br /&gt;
&lt;br /&gt;
Estimating recharge requires a conceptual understanding of the processes that link rainfall to the saturated aquifer. This can be done through two main methods - physically though measurement of water table fluctuations in response to rainfall, or chemically using environmental tracers, where inert rainfall indicators can be tracked via the unsaturated zone or in the groundwater body itself. In Africa both approaches have been used and conjunctive use can be informative although it is often difficult to combine methods for logistical reasons. The main limitations are instrumental, restricting the use of physical measurements of seasonal water levels as well as knowledge of aquifer properties. Similarly some tracer methods are expensive. However the results of research studies involving careful long-term measurement or multiple tracers combined with improved hydrogeological knowledge can be extrapolated to give guidance for more general field application. While it is possible to estimate recharge locally, problems remain in determining the spatial variability of recharge.&lt;br /&gt;
&lt;br /&gt;
Measurements of rainfall flux through the unsaturated zone are widely used for recharge estimation. However physical techniques developed mainly for soil-water studies in an agricultural context are rarely suitable for estimating groundwater recharge. For recharge studies, moisture must pass below a certain depth (often termed the zero-flux plane) where only downward movement takes place. In homogeneous porous sediments, near steady-state movement (piston flow) takes place towards the water table. It is important that measurements of diffuse groundwater recharge only consider data below the zero-flux plane. &lt;br /&gt;
&lt;br /&gt;
In heterogeneous sediments in (semi-)arid terrain, by-pass (macropore or preferential) flow may also be an important process. In older sedimentary formations joints and fractures are naturally present. In some otherwise sandy terrain where carbonate material is present, wetting and drying episodes may lead to mineralisation in and beneath the soil zone, as mineral saturation (especially calcite) is repeatedly exceeded. This is strictly a feature of the zone of fluctuation above the zero-flux plane, however, where calcretes and other near-surface deposits may give rise to hardgrounds with dual porosities. Below a certain depth the pathways of soil macropore movement commonly converge and a more or less homogeneous percolation may be re-established. In some areas, by-pass flow via macropores is found to be significant as in areas of Botswana. Preferential flow may account for at least 50% of fluxes through the unsaturated zone (Beekman et al., 1999; De Vries et al., 2000) and this is verified for example by the presence of tritium at the water table (Beekman et al., 1997).&lt;br /&gt;
&lt;br /&gt;
===Radioactive isotope tracers: Tritium and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl===&lt;br /&gt;
&lt;br /&gt;
Tritium has been widely used in the late 20th century to advance our knowledge of hydrological processes, especially in temperate regions (Zimmerman et al., 1967). It has also been used in a few key studies in (semi-)arid zones to measure recharge rates. In several parts of the world including the Middle East (Edmunds and Walton, 1980; Edmunds et al., 1988), North Africa (Aranyossy and Gaye, 1992; Gaye and Edmunds, 1996) and Australia (Allison and Hughes, 1978), classical profiles from the unsaturated zone show well-defined 1960s tritium peaks some metres below surface, indicating homogeneous movement (piston flow) of water through profiles at relatively low moisture contents (2–4 wt%). These demonstrate that low, but continuous rates of recharge occur in many porous sediments. In some areas dominated by indurated surface layers, deep vegetation or very low rates of recharge, the tritium peak is less well defined (Phillips, 1994), indicating some moisture recycling to greater depths (up to 10 m), although overall penetration of modern water can still be estimated. The usefulness of tritium as a tracer has now largely expired due to radioactive decay (half-life 12.3 years). Nevertheless the evidence and experience from studies in the late 20th century still convey an important lesson. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl (half-life 301,000 years), which also was produced during weapons testing, still offers ways of investigating unsaturated zone processes and recharge although only at a non-routine level. However, in studies where both &amp;lt;sup&amp;gt;3&amp;lt;/sup&amp;gt;H and &amp;lt;sup&amp;gt;36&amp;lt;/sup&amp;gt;Cl have been applied, there is sometimes a discrepancy between recharge indications from the two tracers due to the non-conservative behaviour of tritium (Cook et al., 1994; Phillips, 1999). Nevertheless, the position and shape of the tritium peak in unsaturated zone moisture profiles provides convincing evidence of the extent to which &#039;piston displacement&#039; occurs during recharge, as well as providing reliable estimates of the recharge rate. &lt;br /&gt;
&lt;br /&gt;
===Stable isotopes===&lt;br /&gt;
&lt;br /&gt;
Stable isotopes have been used in the study of recharge but in general only semiquantitative recharge estimates can be obtained. At high rainfall, infiltration undergoes seasonal fractionation within the zone of fluctuation (Darling and Bath, 1988), but this seasonal signal is smoothed out and little variation remains below the top few metres (zero flux plane). In (semi-) arid zones, however, where low recharge rates occur, the record of a sequence of drier years may be recorded as a pulse of 18O-enriched water, as recorded for example from Senegal (Gaye and Edmunds, 1996). This case study (see figure below) illustrates the value of the stable isotope evidence in validating the evidence of other tracers (tritium and chloride)  Extreme isotopic enrichment in the unsaturated zone accompanies chloride accumulation over intervals when recharge rates are zero (Darling et al., 1987) and as illustrated below.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig3.png| 500px | center | thumb| Profiles of tritium, stable isotopes, chloride and nitrate in the unsaturated zone from the same location - profile L18, Louga, Senegal. This profile records the impact of the Sahel drought from 1969 to 1989]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Chloride – diffuse recharge measurement===&lt;br /&gt;
&lt;br /&gt;
Numerous examples of the application of Cl as a conservative tracer in recharge calculations have been published, and Cl mass-balance methods probably offer the most reliable approach to recharge estimation for low rainfall semi-arid and arid regions (Allison et al. 1994; Scanlon et al. 2006 more). Chloride analysis is inexpensive and is widely applicable, bringing it within the budgets of most recharge investigations, although the capacity for accurate measurements of Cl at low concentrations is required. The most common method is the recovery of profiles from unconsolidated sands to provide long-term estimates of recharge at a point source. &lt;br /&gt;
&lt;br /&gt;
The methods of field investigation are straightforward and involve the recovery of samples by dry drilling methods. Techniques used in Africa include augur (up to 45 m), percussion drilling, or by taking samples (up to 70 m) from side walls of dug wells (Bromley et al. ). Samples are immediately sealed in glass jars or polythene bags to avoid moisture loss. Moisture content is measured and chloride extracted by elutriation using demineralised water and then analysed, typically by ion chromatography, calculating pore water concentrations according to the dilution. &lt;br /&gt;
&lt;br /&gt;
A number of criteria must be satisfied or taken into account for successful application: &lt;br /&gt;
&lt;br /&gt;
# surface runoff is minimal&lt;br /&gt;
# Cl is solely derived from rainfall&lt;br /&gt;
# Cl is conservative with no additions from within the aquifer&lt;br /&gt;
# steady-state conditions operate across the unsaturated interval where the method is applied (Edmunds et al. 1988, Herczeg and Edmunds 1999, Wood 1999). &lt;br /&gt;
&lt;br /&gt;
As with tritium, it is important that sampling is made over a depth interval which passes through the zone of fluctuation. &lt;br /&gt;
&lt;br /&gt;
The mean direct recharge rate under steady state conditions is given by the following equation, assuming surface runoff (S) is negligible:&lt;br /&gt;
&lt;br /&gt;
	R= C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;P/C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt; – S&lt;br /&gt;
                                   &lt;br /&gt;
where: &lt;br /&gt;
&lt;br /&gt;
C&amp;lt;sub&amp;gt;R&amp;lt;/sub&amp;gt;	is the mean chloride concentration of moisture below the root zone&lt;br /&gt;
C&amp;lt;sub&amp;gt;P&amp;lt;/sub&amp;gt;	is the weighted mean chloride in total deposition&lt;br /&gt;
P	        is the mean annual rainfall&lt;br /&gt;
S               is the surface runoff&lt;br /&gt;
&lt;br /&gt;
An illustrated example of a chloride mass-balance recharge estimation from a study in Akrotiri, Cyprus is given in the figure below. The sample site was on Quaternary coastal sand dunes with scrub vegetation and mean annual rainfall (P) of 420 mm. Bulked samples were taken every 0.5 m to the water table (except where shown) at 28 m (in later studies samples were taken at 0.25 m using hand augur). Profile shows typical chloride enrichment in the upper 4 m where recycling takes place above the zero flux plane (ZFP). (Some mineralisation may also take place in this zone locking up Cl in closed pore spaces which are then accessed by the destructive sampling technique used.) Below the ZFP a steady-state profile is found with a mean Cl concentration of 200 mg/l. Using the above formula a long term average recharge of about 50 mm/a was derived (Kitching et al., 1980). In this example, oscillations in the Cl correspond with climatic variations and match well the drier and wetter intervals in the second half of the 20th century. A downward moisture flux was estimated at 0.7 m/a. The chemical composition of the groundwater at the water table is comparable to that in the unsaturated zone, suggesting this route is the main source of recharge to the aquifer.&lt;br /&gt;
&lt;br /&gt;
[[File: RC-Fig4.png| 350px | center |thumb  ]]&lt;br /&gt;
&lt;br /&gt;
===Chloride mass-balance methods for groundwater from the saturated zone===&lt;br /&gt;
&lt;br /&gt;
The chloride mass-balance (CMB) approach was originally applied to estimate recharge rates in the saturated zone (Eriksson and Khunakasem, 1969), but there has been less published on this compared with unsaturated zone applications. &lt;br /&gt;
&lt;br /&gt;
A simple application is the study of northern Senegal where the recharge estimates with Cl samples from shallow groundwater (taken from dug wells across a wide area) compare closely with unsaturated zone profiles from the same area, pointing to a homogeneous relationship between the rainfall recharge and the groundwater resource.&lt;br /&gt;
&lt;br /&gt;
In areas where the hydrogeology is heterogeneous with both focused and diffuse recharge components the estimation of recharge using CMB techniques is more complex, and both physical and chemical (tracer) data are required. However if a mass-balance approach is adopted the shallow groundwater chemistry (an integrated record of first arrival of groundwater by mixed pathways) can still provide information on recharge. This is based on the same assumptions (above) as for diffuse recharge. A good conceptual model of the hydrogeology is essential and conjunctive use of physical and chemical approaches is desirable.&lt;br /&gt;
&lt;br /&gt;
A recent example of application of the chloride mass balance to an area of basement in Zimbabwe, the Romwe catchment, is given by MacDonald and Edmunds (2013) where it could be validated with estimates of recharge made using physical methods. Groundwater chemistry (mainly major ion ratios) was used to investigate the relative recharge rates in light and dark bands in the gneiss and to test whether soil type was a good indicator of the underlying geology. The CMB method tested in a control catchment was then used to upscale recharge assessment in a larger area. Over and above the limitations made for the unsaturated zone, the effective rainfall must be measured requiring flow data for the catchment. Some limited agricultural return also needed to be taken into account. Groundwater recharge of 21 mm was derived for the mafic aquifer comparing well with the estimates of 24 mm, made separately, using moisture balance and water table fluctuation methods, respectively. The recharge of 4.4 mm calculated for the felsic aquifer does not compare as well with the corresponding 14 mm using the water table fluctuation method. , However, it supports recharge being higher in the more highly weathered mafic igneous rocks of the basement aquifer and this has a wider significance for resources estimation.&lt;br /&gt;
&lt;br /&gt;
===Physical techniques===&lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water balance&#039;&#039;&#039; approach is a useful physical technique for estimating groundwater recharge. This approach forms the basis for many catchment and groundwater models. In essence, the technique involves accounting for all the water entering or leaving and aquifer.  The equation can be written as:  &lt;br /&gt;
&lt;br /&gt;
R = P + Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; - Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; - ET - &amp;amp;Delta;S - Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt;&lt;br /&gt;
	&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
R is recharge&lt;br /&gt;
&lt;br /&gt;
P is precipitation&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;on&amp;lt;/sub&amp;gt; is runon&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;off&amp;lt;/sub&amp;gt; is runoff&lt;br /&gt;
&lt;br /&gt;
Q&amp;lt;sub&amp;gt;abst&amp;lt;/sub&amp;gt; is groundwater abstraction&lt;br /&gt;
&lt;br /&gt;
ET is evapotranspiration &lt;br /&gt;
&lt;br /&gt;
&amp;amp;Delta;S is change in storage &lt;br /&gt;
&lt;br /&gt;
Each component must be expressed in the same units (e.g. mm/day or m/year).  For an aquifer, the terms on the right hand side of the water budget equation are generally measured or estimated, and&lt;br /&gt;
recharge is calculated as the residual. The disadvantage of the water balance approach is that uncertainties in each of the terms are propagated into the recharge estimate.  The approach is also used to estimate&lt;br /&gt;
recharge using physical lysimeter experiments. Lysimeters are containers filled with soil (disturbed or undisturbed) that are hydrologically isolated from the surrounding soil and used to measure components of the water balance. The inputs and outputs of lysimeter experiments are highly controlled and the method is much more accurate than where unmeasured estimates are used. &lt;br /&gt;
&lt;br /&gt;
The &#039;&#039;&#039;water table fluctuation (WTF)&#039;&#039;&#039; method is based on the premise that rises in groundwater levels in unconfined aquifers are due to recharge water arriving at the water table. Recharge is calculated as (Healy&lt;br /&gt;
and Cook, 2002):&lt;br /&gt;
&lt;br /&gt;
 	&lt;br /&gt;
R = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; dh/dt = S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; Dh/Dt			 &lt;br /&gt;
&lt;br /&gt;
where:&lt;br /&gt;
&lt;br /&gt;
S&amp;lt;sub&amp;gt;y&amp;lt;/sub&amp;gt; is specific yield&lt;br /&gt;
&lt;br /&gt;
h is water table height; and &lt;br /&gt;
&lt;br /&gt;
t is time&lt;br /&gt;
&lt;br /&gt;
The water table fluctuation method is simple to implement, but relies on good estimates of aquifer properties, and can only be applied where there is no groundwater abstraction, or where abstraction can be reliably accounted for.&lt;br /&gt;
&lt;br /&gt;
==Global recharge estimates==&lt;br /&gt;
&lt;br /&gt;
At a global scale, Döll and Fiedler (2008) provide estimates of long term average diffuse groundwater recharge based on the WaterGAP Global Hydrology Model. The model is run with a daily time-step at a spatial resolution of 0.5°, and is driven by gridded precipitation data. Model parameters are adjusted to match observed long-term average river discharge at more than 1000 gauging stations around the world. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Artificial Recharge==&lt;br /&gt;
&lt;br /&gt;
Artificial recharge is the planned, human activity of increasing natural recharge (or infiltration of surface waters into aquifers) with the aim of increasing the amount of groundwater available. Other names for this or related activities are Managed Aquifer Recharge and Aquifer Storage and Recovery. The use of sand dams to artificially increase the potential storage volume for groundwater is one related activity. &lt;br /&gt;
&lt;br /&gt;
Some methods of artificial recharge are simple and have been used for many hundreds or even thousands of years. More technical engineered methods have been used for decades around the world. Artificial recharge or Managed Aquifer Recharge (MAR) technology is flexible and can be applied to many different scales and purposes. However, it can&#039;t be used everywhere - aquifer conditions must be suitable, and there must be excess surface water available to recharge. &lt;br /&gt;
&lt;br /&gt;
Some resources with more information are: &lt;br /&gt;
&lt;br /&gt;
:- [https://www.un-igrac.org/areas-expertise/managed-aquifer-recharge-mar &#039;&#039;&#039;IGRAC - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://recharge.iah.org&#039;&#039;&#039; IAH - Managed Aquifer Recharge&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
:- [https://www.unep.or.jp/ietc/publications/techpublications/techpub-8e/artificial.asp &#039;&#039;&#039;UNEP&#039;&#039;&#039; - Sourcebook of Alternative Technologies for Freshwater Augumentation in Some Countries in Asia (Chapter 3.10: Artificial Recharge of Groundwater)].&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Bonsor HC and MacDonald AM. 2010. [https://nora.nerc.ac.uk/501776/ Groundwater and climate change in Africa: review of recharge studies]. British Geological Survey Internal Report, IR/10/075. &lt;br /&gt;
&lt;br /&gt;
Doll P and Fiedler K. 2008. [https://www.hydrol-earth-syst-sci.net/12/863/2008/hess-12-863-2008.html Global-scale modelling of groundwater recharge]. Hydrology and Earth System Sciences, Vol. 12, 863–885. doi:10.5194/hess-12-863-2008.&lt;br /&gt;
&lt;br /&gt;
Kitching R, Edmunds WM, Shearer TR, Walton NRG and Jacovides J. 1980. Assessment of recharge to aquifers/Evaluation de recharge d&#039;aquiferes. Hydrological Sciences Bulletin 25(3), 217-235. doi:10.1080/02626668009491930 &lt;br /&gt;
 &lt;br /&gt;
Scanlon BR, Healy RW and Cook PG. 2002. [https://link.springer.com/content/pdf/10.1007%2Fs10040-001-0176-2.pdf Choosing appropriate techniques for quantifying groundwater recharge]. Hydrogeology Journal 10, 18–39&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Recharge&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58504</id>
		<title>Aquifer properties</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58504"/>
		<updated>2023-01-30T13:49:29Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Aquifer properties */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; [[Hydrogeological Processes Africa| Key hydrogeological processes]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2023. Aquifer properties. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for updates.&lt;br /&gt;
&lt;br /&gt;
==Aquifer properties==&lt;br /&gt;
&lt;br /&gt;
Aquifer properties are the physical hydraulic characteristics of aquifers. They are quantitative data that are used to describe an aquifer and help understand how groundwater in the aquifer exists and behaves. Aquifer properties are the most important way to describe the hydrogeology of an aquifer. &lt;br /&gt;
&lt;br /&gt;
Key aquifer properties are &#039;&#039;&#039;permeability&#039;&#039;&#039; (or &#039;&#039;&#039;hydraulic conductivity&#039;&#039;&#039;), &#039;&#039;&#039;transmissivity&#039;&#039;&#039;, &#039;&#039;&#039;storativity&#039;&#039;&#039; and &#039;&#039;&#039;specific yield&#039;&#039;&#039;; &#039;&#039;&#039;porosity&#039;&#039;&#039; and &#039;&#039;&#039;specific capacity&#039;&#039;&#039;. &lt;br /&gt;
&lt;br /&gt;
To get reliable information on aquifer properties, aquifer testing must be carried out. Carrying out controlled &#039;&#039;&#039;test pumping&#039;&#039;&#039; of boreholes allows estimates of aquifer thickness, permeability, transmissivity and storage to be made. Without controlled pumping tests, it is not possible to accurately estimate these aquifer properties. The [[Assessing Groundwater Source Yield | &#039;&#039;&#039;assessing source yield&#039;&#039;&#039;]] page gives an overview of pumping tests designed to assess borehole yield; some of these tests can also be used to estimate key aquifer properties, including transmissivity and/or specific capacity. &lt;br /&gt;
&lt;br /&gt;
In many parts of Africa, quantitative aquifer properties data are scarce, and surrogate data and information must be used instead in order to characterise aquifers. The most commonly available hydrogeological data are geology; borehole depth; and borehole yield. Geological and borehole yield data have been used to develop the [[Hydrogeology Map | &#039;&#039;&#039;hydrogeology map&#039;&#039;&#039;]] used in this Atlas. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; [[Hydrogeological Processes Africa| Key hydrogeological processes]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58503</id>
		<title>Aquifer properties</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58503"/>
		<updated>2023-01-30T12:10:51Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; [[Hydrogeological Processes Africa| Key hydrogeological processes]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2023. Aquifer properties. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for updates.&lt;br /&gt;
&lt;br /&gt;
==Aquifer properties==&lt;br /&gt;
&lt;br /&gt;
Aquifer properties are the physical hydraulic characteristics of aquifers. They are quantitative data that are used to describe an aquifer and help understand how groundwater in the aquifer exists and behaves. Aquifer properties are the most important way to describe the hydrogeology of an aquifer. &lt;br /&gt;
&lt;br /&gt;
Key aquifer properties are &#039;&#039;&#039;permeability&#039;&#039;&#039; (or &#039;&#039;&#039;hydraulic conductivity&#039;&#039;&#039;), &#039;&#039;&#039;transmissivity&#039;&#039;&#039;, &#039;&#039;&#039;storativity&#039;&#039;&#039; and &#039;&#039;&#039;specific yield&#039;&#039;&#039;; &#039;&#039;&#039;porosity&#039;&#039;&#039; and &#039;&#039;&#039;specific capacity&#039;&#039;&#039;. &lt;br /&gt;
&lt;br /&gt;
To get reliable information on aquifer properties, aquifer testing must be carried out. Carrying out controlled &#039;&#039;&#039;test pumping&#039;&#039;&#039; of boreholes allows estimates of aquifer thickness, permeability, transmissivity and storage to be made. Without controlled pumping tests, it is not possible to accurately estimate these aquifer properties. The [[Assessing Groundwater Source Yield | &#039;&#039;&#039;assessing source yield&#039;&#039;&#039;]] page gives an overview of pumping tests designed to assess borehole yield; some of these tests can also be used to estimate key aquifer properties, including transmissivity and/or specific capacity. &lt;br /&gt;
&lt;br /&gt;
In many parts of Africa, quantitative aquifer properties data are scarce, and surrogate data and information must be used instead in order to characterise aquifers. The most commonly available hydrogeological data are geology; borehole depth; and borehole yield. Geological and borehole yield data have been used to develop the [[Hydrogeology Map | hydrogeology map]] used in this Atlas. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; [[Hydrogeological Processes Africa| Key hydrogeological processes]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58502</id>
		<title>Aquifer properties</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Aquifer_properties&amp;diff=58502"/>
		<updated>2023-01-30T12:09:56Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Aquifer properties */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Aquifer properties. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for updates.&lt;br /&gt;
&lt;br /&gt;
==Aquifer properties==&lt;br /&gt;
&lt;br /&gt;
Aquifer properties are the physical hydraulic characteristics of aquifers. They are quantitative data that are used to describe an aquifer and help understand how groundwater in the aquifer exists and behaves. Aquifer properties are the most important way to describe the hydrogeology of an aquifer. &lt;br /&gt;
&lt;br /&gt;
Key aquifer properties are &#039;&#039;&#039;permeability&#039;&#039;&#039; (or &#039;&#039;&#039;hydraulic conductivity&#039;&#039;&#039;), &#039;&#039;&#039;transmissivity&#039;&#039;&#039;, &#039;&#039;&#039;storativity&#039;&#039;&#039; and &#039;&#039;&#039;specific yield&#039;&#039;&#039;; &#039;&#039;&#039;porosity&#039;&#039;&#039; and &#039;&#039;&#039;specific capacity&#039;&#039;&#039;. &lt;br /&gt;
&lt;br /&gt;
To get reliable information on aquifer properties, aquifer testing must be carried out. Carrying out controlled &#039;&#039;&#039;test pumping&#039;&#039;&#039; of boreholes allows estimates of aquifer thickness, permeability, transmissivity and storage to be made. Without controlled pumping tests, it is not possible to accurately estimate these aquifer properties. The [[Assessing Groundwater Source Yield | &#039;&#039;&#039;assessing source yield&#039;&#039;&#039;]] page gives an overview of pumping tests designed to assess borehole yield; some of these tests can also be used to estimate key aquifer properties, including transmissivity and/or specific capacity. &lt;br /&gt;
&lt;br /&gt;
In many parts of Africa, quantitative aquifer properties data are scarce, and surrogate data and information must be used instead in order to characterise aquifers. The most commonly available hydrogeological data are geology; borehole depth; and borehole yield. Geological and borehole yield data have been used to develop the [[Hydrogeology Map | hydrogeology map]] used in this Atlas. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Aquifer Properties&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Overview_of_Groundwater_in_Africa&amp;diff=58501</id>
		<title>Overview of Groundwater in Africa</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Overview_of_Groundwater_in_Africa&amp;diff=58501"/>
		<updated>2023-01-30T12:01:36Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Hydrogeological environments in Africa */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages ]] &amp;gt;&amp;gt; Overview of groundwater resources and hydrogeological environments in Africa&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Overview of Groundwater in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater has many advantages as a source of safe, sustainable water in Africa. It is particularly suited to regions with large rural populations, where demand for water is dispersed across large areas. The main advantages and limitations of groundwater as a water resource are summarised below.&lt;br /&gt;
&lt;br /&gt;
====Advantages of groundwater as a water resource in Africa====&lt;br /&gt;
 &lt;br /&gt;
*Groundwater can be found in most environments, at least enough to provide small domestic supplies. It is therefore usually available close to the point of demand.&lt;br /&gt;
*Groundwater usually has excellent natural water quality and is usually suitable for potable use with no prior treatment.&lt;br /&gt;
*Groundwater is naturally more protected from contamination than surface water/&lt;br /&gt;
*Groundwater provides large volumes of natural water storage. Seasonal variations in amount or quality aren&#039;t usually significant, so that groundwater is more drought resistant than surface waters.&lt;br /&gt;
*Groundwater lends itself well to principles of community management. It can be developed incrementally, often at relatively low cost/initial capital investment.&lt;br /&gt;
&lt;br /&gt;
====Limitations of groundwater as a water resource in Africa====&lt;br /&gt;
&lt;br /&gt;
*In some hydrogeological environments, considerable investment is needed to locate and develop suitable sites for groundwater abstraction - dug wells, drilled boreholes or improved springs.&lt;br /&gt;
*In some hydrogeological environments, there can be natural groundwater quality problems - such as iron, fluoride or arsenic.&lt;br /&gt;
*As human development increases, the threat of groundwater pollution increases, and there is a greater need for awareness of, and action on, groundwater and aquifer protection. &lt;br /&gt;
*Groundwater can be vulnerable to over-abstraction, particularly in low productivity aquifers and/or as water demand and the ability to abstract large volumes of water both grow. Long term changes in rainfall patterns can also impact on groundwater recharge and renewal.&lt;br /&gt;
*As overall water supply coverage increases, more hydrogeologically difficult areas can remain unserved, and they become more costly to develop.&lt;br /&gt;
&lt;br /&gt;
===Hydrogeological environments in Africa===&lt;br /&gt;
&lt;br /&gt;
Groundwater is found in [https://en.wikipedia.org/wiki/Aquifer &#039;&#039;&#039;aquifers&#039;&#039;&#039;] - underground layers of water-bearing rock or sediment that contain groundwater. Aquifers are very different in different places, depending on the type and history of rock or sediment of which they are made - ie, depending on their [https://en.wikipedia.org/wiki/Geology &#039;&#039;&#039;geology&#039;&#039;&#039;] and their weathering history.  &lt;br /&gt;
&lt;br /&gt;
How and where groundwater occurs depends primarily on &#039;&#039;&#039;geology&#039;&#039;&#039; (including weathering) and on &#039;&#039;&#039;rainfall&#039;&#039;&#039; (both current and historic). The interaction between these factors gives rise to complex &#039;&#039;&#039;hydrogeological environments&#039;&#039;&#039;, with countless variations in the quantity, quality, ease of access to and renewability of groundwater resources. Because the [https://en.wikipedia.org/wiki/Hydrogeology hydrogeology] - of different hydrogeological environments - in other words, how groundwater exists and behaves - is very different, it is often necessary to use different methods to find, abstract and manage groundwater in different environments. A good understanding of the hydrogeological environment is essential in order to successfully develop groundwater resources. &lt;br /&gt;
&lt;br /&gt;
Africa is hugely diverse in its geology, climate and hydrology. As a result, the hydrogeology of Africa is also hugely variable. But at a continental scale, there are only four main types of &#039;&#039;&#039;hydrogeological environment&#039;&#039;&#039; (or &#039;&#039;&#039;aquifer type&#039;&#039;&#039;) - shown in the map, below: &lt;br /&gt;
&lt;br /&gt;
*&#039;&#039;&#039;basement&#039;&#039;&#039; aquifers; &lt;br /&gt;
*&#039;&#039;&#039;volcanic&#039;&#039;&#039; aquifers; &lt;br /&gt;
*&#039;&#039;&#039;consolidated sedimentary&#039;&#039;&#039; aquifers (which can be dominated by either fracture and/or intergranular flow); and&lt;br /&gt;
*&#039;&#039;&#039;unconsolidated sedimentary&#039;&#039;&#039; aquifers. &lt;br /&gt;
&lt;br /&gt;
A detailed description of these environments is in [https://nora.nerc.ac.uk/501047/ MacDonald and Davies (2001)]; and a summary is below. &lt;br /&gt;
&lt;br /&gt;
[[File:Africa_Hgcl_Envs.png|thumb| 400px|center| The main hydrogeological environments in Africa]] &lt;br /&gt;
&lt;br /&gt;
====Basement aquifers====&lt;br /&gt;
&lt;br /&gt;
Crystalline basement rocks of Precambrian age underlie much of Africa. They form low productivity aquifers that provide small rural water supplies for tens, if not hundreds, of millions of people. Groundwater occurs where the rocks have been significantly weathered and/or in fracture zones, most of which are usually shallower than a few tens of metres depth. Borehole and well yields are generally low, but usually sufficient for rural demand.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:weathered basement.png| 300 px| thumb |left | Groundwater occurrence in a weathered basement aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Volcanic aquifers====&lt;br /&gt;
&lt;br /&gt;
Volcanic rocks underlie a small but significant proportion of Africa&#039;s land area, and are an important water source for tens of millions of people, many of whom live in the drought stricken areas of the Horn of Africa. Groundwater in volcanic aquifers is found within palaeosoils and fractures between lava flows. Yields can be high, and springs are important sources in highland areas.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:volcanic_aquifers.png| 300 px| thumb| right| Groundwater occurrence in a volcanic rock aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Consolidated sedimentary aquifers====&lt;br /&gt;
&lt;br /&gt;
Consolidated sedimentary rocks underlie around one third of Africa&#039;s land area, and can form thick, highly productive aquifers. The most significant aquifers are sandstones and limestones, which can be exploited for large urban as well as rural supplies. Mudstones however, which account for about 65% of all sedimentary rocks in Africa, contain little groundwater, and careful study is required to develop groundwater supplies from mudstones. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:sedimentary_aquifers.png| 300 px| thumb| left | Groundwater occurrence in a consolidated sedimentary aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Unconsolidated sedimentary aquifers====&lt;br /&gt;
&lt;br /&gt;
Unconsolidated sediments directly underlie much of Africa, and are extremely important for both rural and urban water supplies. Unconsolidated sands and gravels occur in most river valleys throughout Africa, and in many coastal areas. These deposits are often highly permeable and can store large volumes of groundwater at shallow depths, which is easy to exploit by traditional shallow wells and boreholes. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:riverside_alluvium.png| 300 px| thumb|  right| Groundwater occurence in unconsolidated valley alluvium]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
===More Information===&lt;br /&gt;
&lt;br /&gt;
More information on geology and aquifer characteristics across Africa can be found in these [[Additional resources | resource pages]]: [[Geology | geology]]; [[Hydrogeology Map | hydrogeology map]]; and [[Aquifer properties| aquifer properties]]. More detailed information on aquifers in each country can be found in the [[Hydrogeology by country | country pages]].&lt;br /&gt;
&lt;br /&gt;
Maps summarising the hydrogeology of Africa: &lt;br /&gt;
[https://www.bgs.ac.uk/research/groundwater/international/africanGroundwater/maps.html Quantitative Groundwater Maps for Africa]&lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M. &amp;amp; Davies, J. 2000. [https://nora.nerc.ac.uk/501047/ A brief review of groundwater for rural water supply in sub-Saharan Africa]. British Geological Survey Report WC/00/033. &lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M., Bonsor, H.C., Ó Dochartaigh, B.É. &amp;amp; Taylor, R.G. 2012. [https://iopscience.iop.org/article/10.1088/1748-9326/7/2/024009;jsessionid=18D8D7F69C3ACBEED0D7494F46850BD6.c1 Quantitative maps of groundwater resources in Africa]. Environmental Research Letters 7(2). &lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M. &amp;amp; Calow, R.C. 2009. [https://nora.nerc.ac.uk/8460/ Developing groundwater for secure water supplies in Africa]. Desalination 248, 546-556. doi: 10.1016/j.desal.2008.05.100&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages ]] &amp;gt;&amp;gt; Overview of Groundwater in Africa&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58500</id>
		<title>Transboundary aquifers</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58500"/>
		<updated>2023-01-30T11:48:48Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Transboundary Aquifers&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for more content. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2019. Transboundary Aquifers. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What are transboundary aquifers?==&lt;br /&gt;
&lt;br /&gt;
Transboundary aquifers (TBAs) are aquifers that underlie more than one country or political region. Management of TBA resources is therefore dependent on cooperation between countries and it is important that they are well understood to ensure they are exploited in a sustainable way. &lt;br /&gt;
&lt;br /&gt;
==Key organisations related to transboundary aquifers==&lt;br /&gt;
&lt;br /&gt;
===[https://www.un-igrac.org/ IGRAC]===&lt;br /&gt;
&lt;br /&gt;
As a United Nations Centre, [https://www.un-igrac.org/ IGRAC] (the International Groundwater Resources Assessment Centre) is the global lead organisation for assessing and providing information on transboundary aquifers, as part of the UNESCO International Hydrological Programme (UNESCO-IHP). There are many initiatives looking at various aspects of transboundary groundwater, including global baseline assessments and more detailed regional or aquifer assessments. Further information can be found on the [https://www.un-igrac.org/areas-expertise/transboundary-groundwaters &#039;&#039;&#039;Transboundary Groundwaters&#039;&#039;&#039;] section of IGRAC&#039;s website. &lt;br /&gt;
&lt;br /&gt;
As part of their work on transboundary aquifers, IGRAC have led the production and publication of a map of Transboundary Aquifers of the World (latest edition 2015), which can be seen in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;]. Based on this global map, they also produced a map of transboundary aquifers of Africa in 2015, which shows the location and extent of all known transboundary aquifers in Africa; and lists the aquifer names, the countries in which they are found, and the area they cover. The map of Africa is designed to encourage further research and assessment of these important water resources. It can be seen online in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;] and a [https://www.un-igrac.org/sites/default/files/resources/files/TBAmap_Africa_2016.pdf &#039;&#039;&#039;pdf version of the Africa map&#039;&#039;&#039;] can be downloaded.&lt;br /&gt;
&lt;br /&gt;
===IWMI===&lt;br /&gt;
&lt;br /&gt;
The [https://wle.cgiar.org/content/international-water-management-institute-iwmi International Water Management Institute] (IWMI), a part of [https://wle.cgiar.org/ CGIAR], developed a map and accompanying inventory of the presently known [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;transboundary aquifers in Africa&#039;&#039;&#039;], in 2013. The map is based on several sources of available data and maps, including global maps by IGRAC and WHYMAP. It shows 80 aquifers or aquifer systems, superimposed on 63 international river or lake basins. The inventory accompanying the map very briefly describes the type of each transboundary aquifer, using inconsistent descriptions that include chronostratigraphic, lithological, rock type (sedimentary, igneous etc), consolidation status, and geological formation names (eg Nubian, Karoo). For each aquifer the inventory also lists the countries that share it, its area, the population living on it, the rainfall it receives annually, and the estimated annual recharge according to the WHYMAP Groundwater Resources Map of Africa. The map is available to download as a [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;pdf file&#039;&#039;&#039;], and is described in detail in the report [https://www.iwmi.cgiar.org/Publications/Other/PDF/transboundary_aquifer_mapping_and_management_in_africa.pdf &#039;&#039;&#039;Transboundary Aquifer Mapping and Management in Africa&#039;&#039;&#039;] (IWMI, 2014).&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Selected projects on specific transboundary aquifers in Africa==&lt;br /&gt;
&lt;br /&gt;
===[https://conjunctivecooperation.iwmi.org/ Conjunctive Water Management for Food Security and Resilience]===&lt;br /&gt;
&lt;br /&gt;
This overall project is a knowledge sharing platform by [https://www.iwmi.cgiar.org/ IWMI], which seeks to capture and disseminate highlights of the increasing knowledge base emerging from work on transboundary river-aquifer systems in the SADC region. Most focus is on three aquifer systems: &lt;br /&gt;
&lt;br /&gt;
* the [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/ &#039;&#039;&#039;Ramotswa-Ngotwane System&#039;&#039;&#039;]. Some outputs from the Ramotswa project can be viewed in the online [https://apps.geodan.nl/igrac/ggis-viewer/viewer/ramotswa/public/default &#039;&#039;&#039;Ramotswa project map portal&#039;&#039;&#039;] hosted by [https://www.un-igrac.org/ IGRAC]. More outputs can be found on the project website [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/reports-and-publications/ &#039;&#039;&#039;Reports and Publications&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
* The [https://sadc-gmi.org/shire-river/ ShireConWat] project (Conjunctive Water Resources Management in the Shire River - Aquifer System). The Shire Aquifer and River Basin System is shared between Malawi and Mozambique. This was run by [https://sadc-gmi.org/ SADC-GMI] as the client and [https://www.iwmi.cgiar.org/ IWMI] as the consultant. Read [https://gripp.iwmi.org/2019/07/04/sadc-member-states-of-malawi-and-mozambique-united-in-commitment-to-transboundary-conjunctive-water-management/ a summary of the project] - at this link you can also access draft versions of these project outputs: a transboundary diagnostic (TDA) to address the issue of system and resource assessment, and a strategic action plan (SAP) to develop the project&#039;s vision and prioritise actions to achieve it.&lt;br /&gt;
&lt;br /&gt;
* The [https://conjunctivecooperation.iwmi.org/tuli-karoo-upper-limpopo-system/ &#039;&#039;&#039;Tuli Karoo-Upper Limpopo System&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 Niger Basin: Support in Groundwater Management to the Niger Basin Authority]===&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is operated by BGR as part of the &#039;&#039;Integrated Water Resources Management ABN&#039;&#039; program of the German Development Cooperation, in partnership with the [https://www.abn.ne/ Niger Basin Authority]. The project aims to implement measures for groundwater protection and sustainable use of groundwater in the Niger Basin Authority&#039;s IWRM (integrated water resources management) programme. Project activities include: &lt;br /&gt;
The project activities include:&lt;br /&gt;
&lt;br /&gt;
* Collection and assessment of groundwater data and maps in the Niger basin to develop a groundwater database and form the basis for a hydrogeological map of the basin&lt;br /&gt;
* Identification of transboundary regions with conflict-ridden groundwater problems&lt;br /&gt;
* Support for measures to improve groundwater management in selected areas&lt;br /&gt;
* Capacity building at all levels (education, training programs, know-how-transfer)&lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 Lake Chad Basin: Groundwater Management]===&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is a joint project between BGR and the Lake Chad Basin Commission, and is the second phase of an initial project [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/abgeschlossen/TZ/Tschad/tschad-I_fb_en.html?nn=1546392 &#039;&#039;&#039;Sustainable Water Management of Lake Chad Basin&#039;&#039;&#039;], which finished in 2011. This second phase has concentrated on the interaction between surface water and groundwater in the inundation plain of the Logone River, which extends from the Lake Chad in the north to the Mandara Mountains in the south of Cameroon. &lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
==Selected other publications==&lt;br /&gt;
&lt;br /&gt;
Scheumann W and Herrfahrdt-Pähle E (Eds.) 2008. [https://www.die-gdi.de/uploads/media/Studie_32.pdf Conceptualizing cooperation on Africa’s transboundary groundwater resources]. German Development Institute (DIE), Bonn. &lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58499</id>
		<title>Transboundary aquifers</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58499"/>
		<updated>2023-01-30T11:47:32Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* Transboundary Aquifers */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Transboundary Aquifers&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for more content. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2019. Transboundary Aquifers. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Transboundary aquifers (TBAs) are aquifers that underlie more than one country or political region. Management of TBA resources is therefore dependent on cooperation between countries and it is important that they are well understood to ensure they are exploited in a sustainable way. &lt;br /&gt;
&lt;br /&gt;
==[https://www.un-igrac.org/ IGRAC]==&lt;br /&gt;
&lt;br /&gt;
As a United Nations Centre, [https://www.un-igrac.org/ IGRAC] (the International Groundwater Resources Assessment Centre) is the global lead organisation for assessing and providing information on transboundary aquifers, as part of the UNESCO International Hydrological Programme (UNESCO-IHP). There are many initiatives looking at various aspects of transboundary groundwater, including global baseline assessments and more detailed regional or aquifer assessments. Further information can be found on the [https://www.un-igrac.org/areas-expertise/transboundary-groundwaters &#039;&#039;&#039;Transboundary Groundwaters&#039;&#039;&#039;] section of IGRAC&#039;s website. &lt;br /&gt;
&lt;br /&gt;
As part of their work on transboundary aquifers, IGRAC have led the production and publication of a map of Transboundary Aquifers of the World (latest edition 2015), which can be seen in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;]. Based on this global map, they also produced a map of transboundary aquifers of Africa in 2015, which shows the location and extent of all known transboundary aquifers in Africa; and lists the aquifer names, the countries in which they are found, and the area they cover. The map of Africa is designed to encourage further research and assessment of these important water resources. It can be seen online in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;] and a [https://www.un-igrac.org/sites/default/files/resources/files/TBAmap_Africa_2016.pdf &#039;&#039;&#039;pdf version of the Africa map&#039;&#039;&#039;] can be downloaded.&lt;br /&gt;
&lt;br /&gt;
==IWMI==&lt;br /&gt;
&lt;br /&gt;
The [https://wle.cgiar.org/content/international-water-management-institute-iwmi International Water Management Institute] (IWMI), a part of [https://wle.cgiar.org/ CGIAR], developed a map and accompanying inventory of the presently known [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;transboundary aquifers in Africa&#039;&#039;&#039;], in 2013. The map is based on several sources of available data and maps, including global maps by IGRAC and WHYMAP. It shows 80 aquifers or aquifer systems, superimposed on 63 international river or lake basins. The inventory accompanying the map very briefly describes the type of each transboundary aquifer, using inconsistent descriptions that include chronostratigraphic, lithological, rock type (sedimentary, igneous etc), consolidation status, and geological formation names (eg Nubian, Karoo). For each aquifer the inventory also lists the countries that share it, its area, the population living on it, the rainfall it receives annually, and the estimated annual recharge according to the WHYMAP Groundwater Resources Map of Africa. The map is available to download as a [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;pdf file&#039;&#039;&#039;], and is described in detail in the report [https://www.iwmi.cgiar.org/Publications/Other/PDF/transboundary_aquifer_mapping_and_management_in_africa.pdf &#039;&#039;&#039;Transboundary Aquifer Mapping and Management in Africa&#039;&#039;&#039;] (IWMI, 2014).&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Selected projects on specific transboundary aquifers in Africa==&lt;br /&gt;
&lt;br /&gt;
===[https://conjunctivecooperation.iwmi.org/ Conjunctive Water Management for Food Security and Resilience]===&lt;br /&gt;
&lt;br /&gt;
This overall project is a knowledge sharing platform by [https://www.iwmi.cgiar.org/ IWMI], which seeks to capture and disseminate highlights of the increasing knowledge base emerging from work on transboundary river-aquifer systems in the SADC region. Most focus is on three aquifer systems: &lt;br /&gt;
&lt;br /&gt;
* the [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/ &#039;&#039;&#039;Ramotswa-Ngotwane System&#039;&#039;&#039;]. Some outputs from the Ramotswa project can be viewed in the online [https://apps.geodan.nl/igrac/ggis-viewer/viewer/ramotswa/public/default &#039;&#039;&#039;Ramotswa project map portal&#039;&#039;&#039;] hosted by [https://www.un-igrac.org/ IGRAC]. More outputs can be found on the project website [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/reports-and-publications/ &#039;&#039;&#039;Reports and Publications&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
* The [https://sadc-gmi.org/shire-river/ ShireConWat] project (Conjunctive Water Resources Management in the Shire River - Aquifer System). The Shire Aquifer and River Basin System is shared between Malawi and Mozambique. This was run by [https://sadc-gmi.org/ SADC-GMI] as the client and [https://www.iwmi.cgiar.org/ IWMI] as the consultant. Read [https://gripp.iwmi.org/2019/07/04/sadc-member-states-of-malawi-and-mozambique-united-in-commitment-to-transboundary-conjunctive-water-management/ a summary of the project] - at this link you can also access draft versions of these project outputs: a transboundary diagnostic (TDA) to address the issue of system and resource assessment, and a strategic action plan (SAP) to develop the project&#039;s vision and prioritise actions to achieve it.&lt;br /&gt;
&lt;br /&gt;
* The [https://conjunctivecooperation.iwmi.org/tuli-karoo-upper-limpopo-system/ &#039;&#039;&#039;Tuli Karoo-Upper Limpopo System&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 Niger Basin: Support in Groundwater Management to the Niger Basin Authority]===&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is operated by BGR as part of the &#039;&#039;Integrated Water Resources Management ABN&#039;&#039; program of the German Development Cooperation, in partnership with the [https://www.abn.ne/ Niger Basin Authority]. The project aims to implement measures for groundwater protection and sustainable use of groundwater in the Niger Basin Authority&#039;s IWRM (integrated water resources management) programme. Project activities include: &lt;br /&gt;
The project activities include:&lt;br /&gt;
&lt;br /&gt;
* Collection and assessment of groundwater data and maps in the Niger basin to develop a groundwater database and form the basis for a hydrogeological map of the basin&lt;br /&gt;
* Identification of transboundary regions with conflict-ridden groundwater problems&lt;br /&gt;
* Support for measures to improve groundwater management in selected areas&lt;br /&gt;
* Capacity building at all levels (education, training programs, know-how-transfer)&lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 Lake Chad Basin: Groundwater Management]===&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is a joint project between BGR and the Lake Chad Basin Commission, and is the second phase of an initial project [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/abgeschlossen/TZ/Tschad/tschad-I_fb_en.html?nn=1546392 &#039;&#039;&#039;Sustainable Water Management of Lake Chad Basin&#039;&#039;&#039;], which finished in 2011. This second phase has concentrated on the interaction between surface water and groundwater in the inundation plain of the Logone River, which extends from the Lake Chad in the north to the Mandara Mountains in the south of Cameroon. &lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
==Selected other publications==&lt;br /&gt;
&lt;br /&gt;
Scheumann W and Herrfahrdt-Pähle E (Eds.) 2008. [https://www.die-gdi.de/uploads/media/Studie_32.pdf Conceptualizing cooperation on Africa’s transboundary groundwater resources]. German Development Institute (DIE), Bonn. &lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58498</id>
		<title>Transboundary aquifers</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58498"/>
		<updated>2023-01-30T11:45:54Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Transboundary Aquifers&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for more content. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2019. Transboundary Aquifers. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Transboundary Aquifers==&lt;br /&gt;
&lt;br /&gt;
Transboundary aquifers (TBAs) are aquifers that underlie more than one country or political region. Management of TBA resources is therefore dependent on cooperation between countries and it is important that they are well understood to ensure they are exploited in a sustainable way. &lt;br /&gt;
&lt;br /&gt;
===IGRAC===&lt;br /&gt;
&lt;br /&gt;
As a United Nations Centre, the International Groundwater Resources Assessment Centre (IGRAC) is taking a global lead on assessing and providing information on transboundary aquifers, as part of the UNESCO International Hydrological Programme (UNESCO-IHP). There are many initiatives looking at various aspects of transboundary groundwater, including global baseline assessments and more detailed regional or aquifer assessments. Further information can be found on the [https://www.un-igrac.org/areas-expertise/transboundary-groundwaters &#039;&#039;&#039;Transboundary Groundwaters&#039;&#039;&#039;] section of IGRAC&#039;s website. &lt;br /&gt;
&lt;br /&gt;
As part of their work on transboundary aquifers, IGRAC have led the production and publication of a map of Transboundary Aquifers of the World (latest edition 2015), which can be seen in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;]. Based on this global map, they also produced a map of transboundary aquifers of Africa in 2015, which shows the location and extent of all known transboundary aquifers in Africa; and lists the aquifer names, the countries in which they are found, and the area they cover. The map of Africa is designed to encourage further research and assessment of these important water resources. It can be seen online in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;] and a [https://www.un-igrac.org/sites/default/files/resources/files/TBAmap_Africa_2016.pdf &#039;&#039;&#039;pdf version of the Africa map&#039;&#039;&#039;] can be downloaded.&lt;br /&gt;
&lt;br /&gt;
===IWMI===&lt;br /&gt;
&lt;br /&gt;
The [https://wle.cgiar.org/content/international-water-management-institute-iwmi International Water Management Institute] (IWMI), a part of [https://wle.cgiar.org/ CGIAR], developed a map and accompanying inventory of the presently known [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;transboundary aquifers in Africa&#039;&#039;&#039;], in 2013. The map is based on several sources of available data and maps, including global maps by IGRAC and WHYMAP. It shows 80 aquifers or aquifer systems, superimposed on 63 international river or lake basins. The inventory accompanying the map very briefly describes the type of each transboundary aquifer, using inconsistent descriptions that include chronostratigraphic, lithological, rock type (sedimentary, igneous etc), consolidation status, and geological formation names (eg Nubian, Karoo). For each aquifer the inventory also lists the countries that share it, its area, the population living on it, the rainfall it receives annually, and the estimated annual recharge according to the WHYMAP Groundwater Resources Map of Africa. The map is available to download as a [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;pdf file&#039;&#039;&#039;], and is described in detail in the report [https://www.iwmi.cgiar.org/Publications/Other/PDF/transboundary_aquifer_mapping_and_management_in_africa.pdf &#039;&#039;&#039;Transboundary Aquifer Mapping and Management in Africa&#039;&#039;&#039;] (IWMI, 2014).&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Selected projects on specific transboundary aquifers in Africa===&lt;br /&gt;
&lt;br /&gt;
====[https://conjunctivecooperation.iwmi.org/ Conjunctive Water Management for Food Security and Resilience]====&lt;br /&gt;
&lt;br /&gt;
This overall project is a knowledge sharing platform by [https://www.iwmi.cgiar.org/ IWMI], which seeks to capture and disseminate highlights of the increasing knowledge base emerging from work on transboundary river-aquifer systems in the SADC region. Most focus is on three aquifer systems: &lt;br /&gt;
&lt;br /&gt;
* the [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/ &#039;&#039;&#039;Ramotswa-Ngotwane System&#039;&#039;&#039;]. Some outputs from the Ramotswa project can be viewed in the online [https://apps.geodan.nl/igrac/ggis-viewer/viewer/ramotswa/public/default &#039;&#039;&#039;Ramotswa project map portal&#039;&#039;&#039;] hosted by [https://www.un-igrac.org/ IGRAC]. More outputs can be found on the project website [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/reports-and-publications/ &#039;&#039;&#039;Reports and Publications&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
* The [https://sadc-gmi.org/shire-river/ ShireConWat] project (Conjunctive Water Resources Management in the Shire River - Aquifer System). The Shire Aquifer and River Basin System is shared between Malawi and Mozambique. This was run by [https://sadc-gmi.org/ SADC-GMI] as the client and [https://www.iwmi.cgiar.org/ IWMI] as the consultant. Read [https://gripp.iwmi.org/2019/07/04/sadc-member-states-of-malawi-and-mozambique-united-in-commitment-to-transboundary-conjunctive-water-management/ a summary of the project] - at this link you can also access draft versions of these project outputs: a transboundary diagnostic (TDA) to address the issue of system and resource assessment, and a strategic action plan (SAP) to develop the project&#039;s vision and prioritise actions to achieve it.&lt;br /&gt;
&lt;br /&gt;
* The [https://conjunctivecooperation.iwmi.org/tuli-karoo-upper-limpopo-system/ &#039;&#039;&#039;Tuli Karoo-Upper Limpopo System&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
====[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 Niger Basin: Support in Groundwater Management to the Niger Basin Authority]====&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is operated by BGR as part of the &#039;&#039;Integrated Water Resources Management ABN&#039;&#039; program of the German Development Cooperation, in partnership with the [https://www.abn.ne/ Niger Basin Authority]. The project aims to implement measures for groundwater protection and sustainable use of groundwater in the Niger Basin Authority&#039;s IWRM (integrated water resources management) programme. Project activities include: &lt;br /&gt;
The project activities include:&lt;br /&gt;
&lt;br /&gt;
* Collection and assessment of groundwater data and maps in the Niger basin to develop a groundwater database and form the basis for a hydrogeological map of the basin&lt;br /&gt;
* Identification of transboundary regions with conflict-ridden groundwater problems&lt;br /&gt;
* Support for measures to improve groundwater management in selected areas&lt;br /&gt;
* Capacity building at all levels (education, training programs, know-how-transfer)&lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
====[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 Lake Chad Basin: Groundwater Management]====&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is a joint project between BGR and the Lake Chad Basin Commission, and is the second phase of an initial project [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/abgeschlossen/TZ/Tschad/tschad-I_fb_en.html?nn=1546392 &#039;&#039;&#039;Sustainable Water Management of Lake Chad Basin&#039;&#039;&#039;], which finished in 2011. This second phase has concentrated on the interaction between surface water and groundwater in the inundation plain of the Logone River, which extends from the Lake Chad in the north to the Mandara Mountains in the south of Cameroon. &lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===Selected other publications===&lt;br /&gt;
&lt;br /&gt;
Scheumann W and Herrfahrdt-Pähle E (Eds.) 2008. [https://www.die-gdi.de/uploads/media/Studie_32.pdf Conceptualizing cooperation on Africa’s transboundary groundwater resources]. German Development Institute (DIE), Bonn. &lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58497</id>
		<title>Transboundary aquifers</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Transboundary_aquifers&amp;diff=58497"/>
		<updated>2023-01-30T11:45:40Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Transboundary Aquifers&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2019. Transboundary Aquifers. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
   This page is still in development. Please check back soon for more content. &lt;br /&gt;
&lt;br /&gt;
==Transboundary Aquifers==&lt;br /&gt;
&lt;br /&gt;
Transboundary aquifers (TBAs) are aquifers that underlie more than one country or political region. Management of TBA resources is therefore dependent on cooperation between countries and it is important that they are well understood to ensure they are exploited in a sustainable way. &lt;br /&gt;
&lt;br /&gt;
===IGRAC===&lt;br /&gt;
&lt;br /&gt;
As a United Nations Centre, the International Groundwater Resources Assessment Centre (IGRAC) is taking a global lead on assessing and providing information on transboundary aquifers, as part of the UNESCO International Hydrological Programme (UNESCO-IHP). There are many initiatives looking at various aspects of transboundary groundwater, including global baseline assessments and more detailed regional or aquifer assessments. Further information can be found on the [https://www.un-igrac.org/areas-expertise/transboundary-groundwaters &#039;&#039;&#039;Transboundary Groundwaters&#039;&#039;&#039;] section of IGRAC&#039;s website. &lt;br /&gt;
&lt;br /&gt;
As part of their work on transboundary aquifers, IGRAC have led the production and publication of a map of Transboundary Aquifers of the World (latest edition 2015), which can be seen in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;]. Based on this global map, they also produced a map of transboundary aquifers of Africa in 2015, which shows the location and extent of all known transboundary aquifers in Africa; and lists the aquifer names, the countries in which they are found, and the area they cover. The map of Africa is designed to encourage further research and assessment of these important water resources. It can be seen online in the [https://ggis.un-igrac.org/ggis-viewer/viewer/tbamap/public/default &#039;&#039;&#039;IGRAC Transboundary aquifers online viewer&#039;&#039;&#039;] and a [https://www.un-igrac.org/sites/default/files/resources/files/TBAmap_Africa_2016.pdf &#039;&#039;&#039;pdf version of the Africa map&#039;&#039;&#039;] can be downloaded.&lt;br /&gt;
&lt;br /&gt;
===IWMI===&lt;br /&gt;
&lt;br /&gt;
The [https://wle.cgiar.org/content/international-water-management-institute-iwmi International Water Management Institute] (IWMI), a part of [https://wle.cgiar.org/ CGIAR], developed a map and accompanying inventory of the presently known [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;transboundary aquifers in Africa&#039;&#039;&#039;], in 2013. The map is based on several sources of available data and maps, including global maps by IGRAC and WHYMAP. It shows 80 aquifers or aquifer systems, superimposed on 63 international river or lake basins. The inventory accompanying the map very briefly describes the type of each transboundary aquifer, using inconsistent descriptions that include chronostratigraphic, lithological, rock type (sedimentary, igneous etc), consolidation status, and geological formation names (eg Nubian, Karoo). For each aquifer the inventory also lists the countries that share it, its area, the population living on it, the rainfall it receives annually, and the estimated annual recharge according to the WHYMAP Groundwater Resources Map of Africa. The map is available to download as a [https://wle.cgiar.org/content/transboundary-aquifer-map-africa &#039;&#039;&#039;pdf file&#039;&#039;&#039;], and is described in detail in the report [https://www.iwmi.cgiar.org/Publications/Other/PDF/transboundary_aquifer_mapping_and_management_in_africa.pdf &#039;&#039;&#039;Transboundary Aquifer Mapping and Management in Africa&#039;&#039;&#039;] (IWMI, 2014).&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Selected projects on specific transboundary aquifers in Africa===&lt;br /&gt;
&lt;br /&gt;
====[https://conjunctivecooperation.iwmi.org/ Conjunctive Water Management for Food Security and Resilience]====&lt;br /&gt;
&lt;br /&gt;
This overall project is a knowledge sharing platform by [https://www.iwmi.cgiar.org/ IWMI], which seeks to capture and disseminate highlights of the increasing knowledge base emerging from work on transboundary river-aquifer systems in the SADC region. Most focus is on three aquifer systems: &lt;br /&gt;
&lt;br /&gt;
* the [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/ &#039;&#039;&#039;Ramotswa-Ngotwane System&#039;&#039;&#039;]. Some outputs from the Ramotswa project can be viewed in the online [https://apps.geodan.nl/igrac/ggis-viewer/viewer/ramotswa/public/default &#039;&#039;&#039;Ramotswa project map portal&#039;&#039;&#039;] hosted by [https://www.un-igrac.org/ IGRAC]. More outputs can be found on the project website [https://conjunctivecooperation.iwmi.org/systems/ramotswa-ngotwane-system/reports-and-publications/ &#039;&#039;&#039;Reports and Publications&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
* The [https://sadc-gmi.org/shire-river/ ShireConWat] project (Conjunctive Water Resources Management in the Shire River - Aquifer System). The Shire Aquifer and River Basin System is shared between Malawi and Mozambique. This was run by [https://sadc-gmi.org/ SADC-GMI] as the client and [https://www.iwmi.cgiar.org/ IWMI] as the consultant. Read [https://gripp.iwmi.org/2019/07/04/sadc-member-states-of-malawi-and-mozambique-united-in-commitment-to-transboundary-conjunctive-water-management/ a summary of the project] - at this link you can also access draft versions of these project outputs: a transboundary diagnostic (TDA) to address the issue of system and resource assessment, and a strategic action plan (SAP) to develop the project&#039;s vision and prioritise actions to achieve it.&lt;br /&gt;
&lt;br /&gt;
* The [https://conjunctivecooperation.iwmi.org/tuli-karoo-upper-limpopo-system/ &#039;&#039;&#039;Tuli Karoo-Upper Limpopo System&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
====[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 Niger Basin: Support in Groundwater Management to the Niger Basin Authority]====&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is operated by BGR as part of the &#039;&#039;Integrated Water Resources Management ABN&#039;&#039; program of the German Development Cooperation, in partnership with the [https://www.abn.ne/ Niger Basin Authority]. The project aims to implement measures for groundwater protection and sustainable use of groundwater in the Niger Basin Authority&#039;s IWRM (integrated water resources management) programme. Project activities include: &lt;br /&gt;
The project activities include:&lt;br /&gt;
&lt;br /&gt;
* Collection and assessment of groundwater data and maps in the Niger basin to develop a groundwater database and form the basis for a hydrogeological map of the basin&lt;br /&gt;
* Identification of transboundary regions with conflict-ridden groundwater problems&lt;br /&gt;
* Support for measures to improve groundwater management in selected areas&lt;br /&gt;
* Capacity building at all levels (education, training programs, know-how-transfer)&lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Niger/abn_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
====[https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 Lake Chad Basin: Groundwater Management]====&lt;br /&gt;
&lt;br /&gt;
This project, which finishes in 2022, is a joint project between BGR and the Lake Chad Basin Commission, and is the second phase of an initial project [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/abgeschlossen/TZ/Tschad/tschad-I_fb_en.html?nn=1546392 &#039;&#039;&#039;Sustainable Water Management of Lake Chad Basin&#039;&#039;&#039;], which finished in 2011. This second phase has concentrated on the interaction between surface water and groundwater in the inundation plain of the Logone River, which extends from the Lake Chad in the north to the Mandara Mountains in the south of Cameroon. &lt;br /&gt;
&lt;br /&gt;
More information, and the download of project reports, maps and other outputs, is on the [https://www.deutscher-rohstoffeffizienz-preis.de/EN/Themen/Wasser/Projekte/laufend/TZ/Tschad/tschad-II_fb_en.html?nn=1546392 &#039;&#039;&#039;project website&#039;&#039;&#039;].&lt;br /&gt;
&lt;br /&gt;
===Selected other publications===&lt;br /&gt;
&lt;br /&gt;
Scheumann W and Herrfahrdt-Pähle E (Eds.) 2008. [https://www.die-gdi.de/uploads/media/Studie_32.pdf Conceptualizing cooperation on Africa’s transboundary groundwater resources]. German Development Institute (DIE), Bonn. &lt;br /&gt;
&lt;br /&gt;
Return to: [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Key_Groundwater_Issues&amp;diff=58496</id>
		<title>Key Groundwater Issues</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Key_Groundwater_Issues&amp;diff=58496"/>
		<updated>2023-01-30T11:45:06Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]  &amp;gt;&amp;gt; Key Groundwater Issues&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
A series of pages covering key issues relating to groundwater in Africa.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==[[Groundwater quality in Africa | Groundwater quality]]==&lt;br /&gt;
&lt;br /&gt;
Groundwater quality is a key issue in developing and managing groundwater resources. The [[Groundwater quality in Africa | &#039;&#039;&#039;groundwater quality&#039;&#039;&#039;]] page gives background on some of the main issues related to groundwater quality in Africa, including overviews of groundwater quality in some countries, and natural (geogenic) and pollutant causes of poor groundwater quality.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==[[Urban groundwater in Africa | Urban groundwater in Africa]]==&lt;br /&gt;
&lt;br /&gt;
Groundwater is already a vital resource in towns and cities across Africa, and is becoming ever more important as the pace of urbanisation grows. The development, management and protection of groundwater resources in urban areas faces additional challenges to that in rural areas. The [[Urban groundwater in Africa | &#039;&#039;&#039;Urban groundwater in Africa&#039;&#039;&#039;]] page provides some background on issues relating to urban groundwater in Africa, and links to more information.&lt;br /&gt;
 &lt;br /&gt;
&lt;br /&gt;
==[[Groundwater irrigation in Africa | Groundwater and irrigation in Africa]]==&lt;br /&gt;
&lt;br /&gt;
Currently only about 1% of cultivated land in Africa is irrigated using groundwater. Most irrigation using groundwater in Africa is at small scales by smallholder farmers, but there are large scale groundwater irrigation schemes in some countries, particularly in South Africa and in north African countries. Irrigation can significantly improve food security and improvements in livelihoods, and groundwater can play a major role in this in future, if sustainably managed. The [[Groundwater irrigation in Africa | &#039;&#039;&#039;Groundwater and irrigation in Africa&#039;&#039;&#039;]] page provides some background, and links to more information, including case studies.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==[[Transboundary aquifers | Transboundary aquifers]]==&lt;br /&gt;
&lt;br /&gt;
Transboundary aquifers underlie more than one country or political region. The management of transboundary aquifers requires cooperation between countries. The [[Transboundary aquifers | &#039;&#039;&#039;Transboundary aquifers&#039;&#039;&#039;]] page gives some background on mapping transboundary aquifers across Africa, and some large scale projects to increase understanding of major transboundary aquifers, such as the Lake Chad Basin. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource Pages]] &lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58495</id>
		<title>Additional resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58495"/>
		<updated>2023-01-30T11:34:12Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Information resources on groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
These pages provide background information on many different aspects of groundwater and hydrogeology, with particular relevance to Africa, and links to more detailed resources. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Overview_of_Groundwater_in_Africa| An overview of groundwater in Africa]]===&lt;br /&gt;
&lt;br /&gt;
A brief [[Overview_of_Groundwater_in_Africa| background to groundwater resources and hydrogeological environments in Africa]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
These pages have information on the geological and other environmental maps and graphs on the country pages: how they were developed, and links to original data sources.&lt;br /&gt;
&lt;br /&gt;
:- [[Geography| Country boundaries and land surface elevation]]&lt;br /&gt;
&lt;br /&gt;
:- [[Geology  | Geology]]&lt;br /&gt;
&lt;br /&gt;
:- [[Climate | Climate]]&lt;br /&gt;
&lt;br /&gt;
:- [[Land cover | Land cover]]&lt;br /&gt;
&lt;br /&gt;
:- [[Soil | Soil]] &lt;br /&gt;
&lt;br /&gt;
:- [[Surface water | Surface water]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeological Processes Africa| Key hydrogeological processes]]===&lt;br /&gt;
&lt;br /&gt;
An overview of key hydrogeological processes, with particular relevance to Africa: &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology Maps Of Africa | Overview of groundwater and hydrogeological maps of Africa]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Hydrogeology Maps Of Africa | Groundwater and hydrogeological maps of Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa Groundwater Atlas Hydrogeology Maps | The Africa Groundwater Atlas country hydrogeology maps]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Developing groundwater resources | Developing groundwater resources]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater development techniques | Introduction to groundwater development procedures]]&lt;br /&gt;
&lt;br /&gt;
:- [[Borehole Drilling | Borehole Drilling]], including professionalising drilling&lt;br /&gt;
&lt;br /&gt;
:- [[Manual drilling | Manual drilling]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes | Siting Boreholes]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes:Reconnaissance | Siting Boreholes:Reconnaissance]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Groundwater Source Yield |Assessing source yield]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Water Quality | Assessing water quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Management | Groundwater management]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater management organisations | Groundwater management organisations]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater Data | Groundwater data]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater use | Groundwater use in Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Data | Groundwater data]]===&lt;br /&gt;
&lt;br /&gt;
Information on and links to sources of [[Groundwater Data | groundwater data]] in Africa.&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa National Groundwater Databases | &#039;&#039;&#039;Inventory of national groundwater databases in Africa&#039;&#039;&#039;]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Key Groundwater Issues | Key groundwater issues]]===&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
:-[[Urban groundwater in Africa | Urban groundwater in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater irrigation in Africa | Groundwater and irrigation in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Transboundary aquifers | Transboundary aquifers]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Case studies===&lt;br /&gt;
&lt;br /&gt;
:- A series of [[Case studies | &#039;&#039;&#039;case studies&#039;&#039;&#039;]] that illustrate different groundwater understanding and management issues across Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Research in Africa | Groundwater Research in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Information on key current and past groundwater research themes and projects in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Educational Resources | Groundwater Training and Educational Resources]]===&lt;br /&gt;
&lt;br /&gt;
Information and resources on online training courses and course material for water professionals, and educational resources to help explain groundwater issues and hydrogeology.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Organisations in Africa | Groundwater Organisations in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Links to some of the  many professional networks and organisations offer support to those working in groundwater and hydrogeology in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58494</id>
		<title>Additional resources</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Additional_resources&amp;diff=58494"/>
		<updated>2023-01-30T11:34:03Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
For each country, the Atlas provides maps and graphs with information on environmental parameters closely related to groundwater: [[Geology  | &#039;&#039;geology&#039;&#039;]], [[Climate | &#039;&#039;climate&#039;&#039;]], [[Surface water | &#039;&#039;major rivers&#039;&#039;]], [[Soil | &#039;&#039;soils&#039;&#039;]] and [[Land cover | &#039;&#039;land cover&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Information resources on groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
These pages provide background information on many different aspects of groundwater and hydrogeology, with particular relevance to Africa, and links to more detailed resources. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Overview_of_Groundwater_in_Africa| An overview of groundwater in Africa]]===&lt;br /&gt;
&lt;br /&gt;
A brief [[Overview_of_Groundwater_in_Africa| background to groundwater resources and hydrogeological environments in Africa]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
These pages have information on the geological and other environmental maps and graphs on the country pages: how they were developed, and links to original data sources.&lt;br /&gt;
&lt;br /&gt;
:- [[Geography| Country boundaries and land surface elevation]]&lt;br /&gt;
&lt;br /&gt;
:- [[Geology  | Geology]]&lt;br /&gt;
&lt;br /&gt;
:- [[Climate | Climate]]&lt;br /&gt;
&lt;br /&gt;
:- [[Land cover | Land cover]]&lt;br /&gt;
&lt;br /&gt;
:- [[Soil | Soil]] &lt;br /&gt;
&lt;br /&gt;
:- [[Surface water | Surface water]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeological Processes Africa| Key hydrogeological processes]]===&lt;br /&gt;
&lt;br /&gt;
An overview of key hydrogeological processes, with particular relevance to Africa: &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology Maps Of Africa | Overview of groundwater and hydrogeological maps of Africa]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Hydrogeology Maps Of Africa | Groundwater and hydrogeological maps of Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa Groundwater Atlas Hydrogeology Maps | The Africa Groundwater Atlas country hydrogeology maps]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Developing groundwater resources | Developing groundwater resources]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater development techniques | Introduction to groundwater development procedures]]&lt;br /&gt;
&lt;br /&gt;
:- [[Borehole Drilling | Borehole Drilling]], including professionalising drilling&lt;br /&gt;
&lt;br /&gt;
:- [[Manual drilling | Manual drilling]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes | Siting Boreholes]]&lt;br /&gt;
&lt;br /&gt;
:- [[Siting Boreholes:Reconnaissance | Siting Boreholes:Reconnaissance]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Groundwater Source Yield |Assessing source yield]]&lt;br /&gt;
&lt;br /&gt;
:- [[Assessing Water Quality | Assessing water quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Management | Groundwater management]]===&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater management organisations | Groundwater management organisations]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater Data | Groundwater data]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater use | Groundwater use in Africa]]&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Data | Groundwater data]]===&lt;br /&gt;
&lt;br /&gt;
Information on and links to sources of [[Groundwater Data | groundwater data]] in Africa.&lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater monitoring | Groundwater monitoring]]&lt;br /&gt;
&lt;br /&gt;
:- [[Africa National Groundwater Databases | &#039;&#039;&#039;Inventory of national groundwater databases in Africa&#039;&#039;&#039;]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Key Groundwater Issues | Key groundwater issues]]===&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater quality in Africa | Groundwater quality]]&lt;br /&gt;
&lt;br /&gt;
:-[[Urban groundwater in Africa | Urban groundwater in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Groundwater irrigation in Africa | Groundwater and irrigation in Africa]]&lt;br /&gt;
&lt;br /&gt;
:-[[Transboundary aquifers | Transboundary aquifers]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Case studies===&lt;br /&gt;
&lt;br /&gt;
:- A series of [[Case studies | &#039;&#039;&#039;case studies&#039;&#039;&#039;]] that illustrate different groundwater understanding and management issues across Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Research in Africa | Groundwater Research in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Information on key current and past groundwater research themes and projects in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Educational Resources | Groundwater Training and Educational Resources]]===&lt;br /&gt;
&lt;br /&gt;
Information and resources on online training courses and course material for water professionals, and educational resources to help explain groundwater issues and hydrogeology.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Organisations in Africa | Groundwater Organisations in Africa]]===&lt;br /&gt;
&lt;br /&gt;
Links to some of the  many professional networks and organisations offer support to those working in groundwater and hydrogeology in Africa. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; Resource Pages&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Groundwater_in_Africa&amp;diff=58493</id>
		<title>Groundwater in Africa</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Groundwater_in_Africa&amp;diff=58493"/>
		<updated>2023-01-30T11:30:00Z</updated>

		<summary type="html">&lt;p&gt;Beod: Blanked the page&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Hydrogeological_Processes_Africa&amp;diff=58492</id>
		<title>Hydrogeological Processes Africa</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Hydrogeological_Processes_Africa&amp;diff=58492"/>
		<updated>2023-01-30T11:29:49Z</updated>

		<summary type="html">&lt;p&gt;Beod: Created page with &amp;quot; Africa Groundwater Atlas &amp;gt;&amp;gt;  Resource pages &amp;gt;&amp;gt; Key hydrogeological processes, with particular reference to Africa    This page is still being developed. Please check back soon for more information.  ==Key hydrogeological processes==  These pages provide background on the hydrogeological processes that are an essential part of understanding groundwater resources and hydrogeology, and specific information releva...&amp;quot;&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Key hydrogeological processes, with particular reference to Africa&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
==Key hydrogeological processes==&lt;br /&gt;
&lt;br /&gt;
These pages provide background on the hydrogeological processes that are an essential part of understanding groundwater resources and hydrogeology, and specific information relevant to Africa. &lt;br /&gt;
&lt;br /&gt;
:- [[Aquifer properties | Aquifer properties]]&lt;br /&gt;
&lt;br /&gt;
:- [[Recharge | Recharge]] &lt;br /&gt;
&lt;br /&gt;
:- [[Groundwater quality in Africa | Groundwater quality and groundwater chemistry]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]]&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Africa_Groundwater_Atlas_Home&amp;diff=58491</id>
		<title>Africa Groundwater Atlas Home</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Africa_Groundwater_Atlas_Home&amp;diff=58491"/>
		<updated>2023-01-30T11:27:19Z</updated>

		<summary type="html">&lt;p&gt;Beod: /*  Resource pages */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;{| class = &amp;quot;wikitable&amp;quot;&lt;br /&gt;
|+ &lt;br /&gt;
||[[File:(col)_bgs.jpg  | 200px]]&lt;br /&gt;
&lt;br /&gt;
||[[File:Logo colour.png |100px]]&lt;br /&gt;
&lt;br /&gt;
||[[File:UPGro Logo.png | 100px]]&lt;br /&gt;
&lt;br /&gt;
||[[File:idslogo.png | 100px]]&lt;br /&gt;
&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
   &#039;&#039;&#039;[[Atlas Eaux Souterraines Afrique | Lire l&#039;Atlas des eaux souterraines d l&#039;Afrique en français]]&#039;&#039;&#039;  [[File: flag_of_france.png  | 50px]]&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Welcome to the Africa Groundwater Atlas==&lt;br /&gt;
&lt;br /&gt;
This Atlas provides a summary of the hydrogeology and groundwater resources of 51 African countries, and a gateway to further information. The aim of the Atlas is to improve the availability and accessibility of high quality information on groundwater in Africa, to support the safe and sustainable development and use of groundwater resources. &lt;br /&gt;
&lt;br /&gt;
As well as information on individual countries, Atlas provides links to further information, including through the [https://www.bgs.ac.uk/africagroundwateratlas/index.cfm Africa Groundwater Literature Archive], and also provides supporting information on many groundwater-related issues that affect sustainable groundwater development, management and use.&lt;br /&gt;
&lt;br /&gt;
The Atlas provides groundwater information and maps at a national scale, not local, site-specific groundwater information. For site-specific groundwater assessments, such as siting new water boreholes, more detailed information is needed.&lt;br /&gt;
&lt;br /&gt;
==Hydrogeology and groundwater resources by country==&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology by country | Hydrogeology by country]]===&lt;br /&gt;
&lt;br /&gt;
The [[Hydrogeology by country | &#039;&#039;&#039;Hydrogeology by country&#039;&#039;&#039;]] section provides a profile of each of 51 countries in Africa, and a gateway to further information sources. Each country page provides a summary of the geology and hydrogeology of key aquifers, the status of groundwater resources, and groundwater management. For each country there is also [[Supporting environmental information | supporting environmental information]]: climate, major rivers, soils and land cover. &lt;br /&gt;
&lt;br /&gt;
[[File:AGA_Overview.png | 400px | center ]]&lt;br /&gt;
&lt;br /&gt;
===[[List of Authors | Contributing authors]]===&lt;br /&gt;
&lt;br /&gt;
The country profiles were prepared by the British Geological Survey (BGS) in collaboration with hydrogeologists, geologists and other groundwater experts from across Africa and beyond. The authors are cited on the relevant country pages, and details of all the [[List of Authors | &#039;&#039;&#039;contributing authors&#039;&#039;&#039; ]] can be found here.&lt;br /&gt;
&lt;br /&gt;
==[[Additional resources | Resource pages]]==&lt;br /&gt;
&lt;br /&gt;
This section provides a series of pages with additional information on key issues related to hydrogeology, groundwater resources and management in Africa.&lt;br /&gt;
&lt;br /&gt;
===[[Overview_of_Groundwater_in_Africa| An overview of groundwater in Africa]]===&lt;br /&gt;
&lt;br /&gt;
A brief [[Overview_of_Groundwater_in_Africa| background to groundwater resources and hydrogeological environments in Africa]]&lt;br /&gt;
&lt;br /&gt;
===[[Supporting environmental information | Supporting geological and environmental information]]===&lt;br /&gt;
&lt;br /&gt;
For each country, the Atlas provides maps and graphs with information on environmental parameters closely related to groundwater: [[Geology  | &#039;&#039;geology&#039;&#039;]], [[Climate | &#039;&#039;climate&#039;&#039;]], [[Surface water | &#039;&#039;major rivers&#039;&#039;]], [[Soil | &#039;&#039;soils&#039;&#039;]] and [[Land cover | &#039;&#039;land cover&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeological Processes Africa| Key hydrogeological processes]]===&lt;br /&gt;
&lt;br /&gt;
An overview of key hydrogeological processes, with particular relevance to Africa: [[Aquifer properties | &#039;&#039;aquifer properties&#039;&#039;]], [[Recharge | &#039;&#039;recharge&#039;&#039;]], and [[Groundwater quality in Africa | &#039;&#039;groundwater quality&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
===[[Hydrogeology Maps Of Africa | Groundwater and Hydrogeological Maps of Africa]]===&lt;br /&gt;
&lt;br /&gt;
Information on [[Hydrogeology Maps Of Africa | &#039;&#039;maps of groundwater and hydrogeology of Africa&#039;&#039;]], including the [[Africa Groundwater Atlas Hydrogeology Maps | &#039;&#039;Africa Groundwater Atlas &#039;&#039;&#039;Country Hydrogeology Maps&#039;&#039;&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
===[[Developing Groundwater Resources | Developing groundwater resources (groundwater development)]] ===&lt;br /&gt;
&lt;br /&gt;
Resources relating to the sustainable development of groundwater resources using different [[Groundwater source types | &#039;&#039;groundwater source types&#039;&#039;]], including [[Stages in groundwater exploration | &#039;&#039;stages and techniques for groundwater exploration and development&#039;&#039;]], such as [[Siting Boreholes | &#039;&#039;siting boreholes&#039;&#039;]], [[Borehole Drilling | &#039;&#039;borehole drilling&#039;&#039;]], [[Manual drilling | &#039;&#039;manual drilling&#039;&#039;]],  [[Assessing Groundwater Source Yield | &#039;&#039;assessing source yield&#039;&#039;]] and [[Assessing Water Quality | &#039;&#039;assessing groundwater quality&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Management | Groundwater management]]===&lt;br /&gt;
&lt;br /&gt;
Organisations supporting groundwater management; information on [[Groundwater monitoring | &#039;&#039;groundwater monitoring&#039;&#039;]], [[Groundwater use | &#039;&#039;groundwater use&#039;&#039;]] and [[Groundwater Data | &#039;&#039;groundwater data&#039;&#039;]] in Africa.&lt;br /&gt;
&lt;br /&gt;
===[[Key Groundwater Issues | Key groundwater issues]]===&lt;br /&gt;
&lt;br /&gt;
Information on key groundwater issues in Africa, including [[Urban groundwater in Africa | &#039;&#039;urban groundwater&#039;&#039;]], [[Groundwater irrigation in Africa | &#039;&#039;groundwater and irrigation&#039;&#039;]], [[Groundwater quality in Africa | &#039;&#039;groundwater quality&#039;&#039;]] and [[Transboundary aquifers | &#039;&#039;transboundary aquifers&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
===[[Case studies | Case studies]]===&lt;br /&gt;
&lt;br /&gt;
These [[Case studies | case studies]] give practical examples of groundwater issues and how they have been addressed in countries across Africa.&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Data | Groundwater Data]]===&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Research in Africa | Groundwater Research in Africa]]===&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Educational Resources | Training and Educational Resources]]===&lt;br /&gt;
&lt;br /&gt;
Information and resources on online training courses and course material for water professionals, and educational resources to help explain groundwater issues and hydrogeology.&lt;br /&gt;
&lt;br /&gt;
===[[Groundwater Organisations in Africa | Groundwater Organisations in Africa]]===&lt;br /&gt;
&lt;br /&gt;
==[https://www.bgs.ac.uk/africagroundwateratlas/archive.cfm Africa Groundwater Literature Archive]==&lt;br /&gt;
&lt;br /&gt;
The [https://www.bgs.ac.uk/africagroundwateratlas/archive.cfm &#039;&#039;&#039;Africa Groundwater Literature Archive&#039;&#039;&#039;] &lt;br /&gt;
is is an online library of documents about groundwater in Africa - a searchable database holding bibliographic references for thousands of items of literature related to groundwater in Africa. The documents include published and unpublished reports, journal papers, maps, books and academic theses. &lt;br /&gt;
&lt;br /&gt;
Search the Archive by:&lt;br /&gt;
&lt;br /&gt;
:-  &#039;&#039;&#039;location&#039;&#039;&#039; - search for all documents for a particular country; or for many of the documents, search for their detailed location on a map.&lt;br /&gt;
:- thematic &#039;&#039;&#039;keyword&#039;&#039;&#039; - for example, search for documents about &#039;&#039;aquifer characterisation&#039;&#039;, &#039;&#039;groundwater quality&#039;&#039;, or &#039;&#039;socio-economics&#039;&#039;&lt;br /&gt;
&lt;br /&gt;
The Archive gives full bibliographic references and, whereever possible, links to full-text documents. &lt;br /&gt;
&lt;br /&gt;
[[Africa Groundwater Literature Archive description | &#039;&#039;&#039;Background information about the Africa Groundwater Literature Archive project&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
[[File:Archivefront.PNG | 400px | center ]]&lt;br /&gt;
&lt;br /&gt;
==Background to the Africa Groundwater Atlas==&lt;br /&gt;
&lt;br /&gt;
===Further project information===&lt;br /&gt;
&lt;br /&gt;
[[Africa_Groundwater_Atlas_description| &#039;&#039;&#039;Further information&#039;&#039;&#039;]] on the Africa Groundwater Atlas project. &lt;br /&gt;
&lt;br /&gt;
===Terms of use===&lt;br /&gt;
&lt;br /&gt;
[[Africa Groundwater Atlas Terms of Use | &#039;&#039;&#039;Terms of use&#039;&#039;&#039;]] for information provided in the Atlas.&lt;br /&gt;
&lt;br /&gt;
===Contact us===&lt;br /&gt;
&lt;br /&gt;
If you would like further information about the Africa Groundwater Atlas, or have groundwater information you would like to see added to the Atlas, please contact us at [mailto:AfricaGWAtlas@bgs.ac.uk  AfricaGWAtlas@bgs.ac.uk].&lt;br /&gt;
&lt;br /&gt;
==[[Wikipedia edit-a-thon | Wikipedia edit-a-thon]]==&lt;br /&gt;
&lt;br /&gt;
At the 2019 IAH Congress we ran a [[Wikipedia edit-a-thon | Wikipedia edit-a-thon]] to transfer content from the Africa Groundwater Atlas into Wikipedia, to create the first Groundwater in Africa Wikipedia pages - making hydrogeology information for Africa even more visible and accessible to a wider audience. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&amp;lt;!--        PLEASE DO NOT DELETE BELOW THIS LINE        --&amp;gt;&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Overview_of_Groundwater_in_Africa&amp;diff=58490</id>
		<title>Overview of Groundwater in Africa</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Overview_of_Groundwater_in_Africa&amp;diff=58490"/>
		<updated>2023-01-30T11:23:07Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages ]] &amp;gt;&amp;gt; Overview of groundwater resources and hydrogeological environments in Africa&lt;br /&gt;
&lt;br /&gt;
 Please cite page as: Africa Groundwater Atlas. 2019. Overview of Groundwater in Africa. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Groundwater in Africa==&lt;br /&gt;
&lt;br /&gt;
Groundwater has many advantages as a source of safe, sustainable water in Africa. It is particularly suited to regions with large rural populations, where demand for water is dispersed across large areas. The main advantages and limitations of groundwater as a water resource are summarised below.&lt;br /&gt;
&lt;br /&gt;
====Advantages of groundwater as a water resource in Africa====&lt;br /&gt;
 &lt;br /&gt;
*Groundwater can be found in most environments, at least enough to provide small domestic supplies. It is therefore usually available close to the point of demand.&lt;br /&gt;
*Groundwater usually has excellent natural water quality and is usually suitable for potable use with no prior treatment.&lt;br /&gt;
*Groundwater is naturally more protected from contamination than surface water/&lt;br /&gt;
*Groundwater provides large volumes of natural water storage. Seasonal variations in amount or quality aren&#039;t usually significant, so that groundwater is more drought resistant than surface waters.&lt;br /&gt;
*Groundwater lends itself well to principles of community management. It can be developed incrementally, often at relatively low cost/initial capital investment.&lt;br /&gt;
&lt;br /&gt;
====Limitations of groundwater as a water resource in Africa====&lt;br /&gt;
&lt;br /&gt;
*In some hydrogeological environments, considerable investment is needed to locate and develop suitable sites for groundwater abstraction - dug wells, drilled boreholes or improved springs.&lt;br /&gt;
*In some hydrogeological environments, there can be natural groundwater quality problems - such as iron, fluoride or arsenic.&lt;br /&gt;
*As human development increases, the threat of groundwater pollution increases, and there is a greater need for awareness of, and action on, groundwater and aquifer protection. &lt;br /&gt;
*Groundwater can be vulnerable to over-abstraction, particularly in low productivity aquifers and/or as water demand and the ability to abstract large volumes of water both grow. Long term changes in rainfall patterns can also impact on groundwater recharge and renewal.&lt;br /&gt;
*As overall water supply coverage increases, more hydrogeologically difficult areas can remain unserved, and they become more costly to develop.&lt;br /&gt;
&lt;br /&gt;
===Hydrogeological environments in Africa===&lt;br /&gt;
&lt;br /&gt;
How and where groundwater occurs depends primarily on &#039;&#039;&#039;geology&#039;&#039;&#039;, &#039;&#039;&#039;geomorphology/weathering&#039;&#039;&#039;, and &#039;&#039;&#039;rainfall&#039;&#039;&#039; (both current and historic). The interaction between these three factors gives rise to complex hydrogeological environments, with countless variations in the quantity, quality, ease of access to and renewability of groundwater resources. Because the hydrogeology - how groundwater exists and behaves - is different in each environment, different methods are needed to find, abstract and manage groundwater. Successfully developing groundwater resources depends on a good understanding of the hydrogeological environment. &lt;br /&gt;
&lt;br /&gt;
Africa is hugely diverse in its geology, climate and hydrology. As a result, the hydrogeology of Africa is also hugely variable. But at a continental scale, there are only four main types of &#039;&#039;&#039;hydrogeological environment&#039;&#039;&#039; (or &#039;&#039;&#039;aquifer type&#039;&#039;&#039;) - shown in the map, below: &lt;br /&gt;
&lt;br /&gt;
*&#039;&#039;&#039;basement&#039;&#039;&#039; aquifers; &lt;br /&gt;
*&#039;&#039;&#039;volcanic&#039;&#039;&#039; aquifers; &lt;br /&gt;
*&#039;&#039;&#039;consolidated sedimentary&#039;&#039;&#039; aquifers (which can be dominated by either fracture and/or intergranular flow); and&lt;br /&gt;
*&#039;&#039;&#039;unconsolidated sedimentary&#039;&#039;&#039; aquifers. &lt;br /&gt;
&lt;br /&gt;
A detailed description of these environments is in [https://nora.nerc.ac.uk/501047/ MacDonald and Davies (2001)]; and a summary is below. &lt;br /&gt;
&lt;br /&gt;
[[File:Africa_Hgcl_Envs.png|thumb| 400px|center| The main hydrogeological environments in Africa]] &lt;br /&gt;
&lt;br /&gt;
====Basement aquifers====&lt;br /&gt;
&lt;br /&gt;
Crystalline basement rocks of Precambrian age underlie much of Africa. They form low productivity aquifers that provide small rural water supplies for tens, if not hundreds, of millions of people. Groundwater occurs where the rocks have been significantly weathered and/or in fracture zones, most of which are usually shallower than a few tens of metres depth. Borehole and well yields are generally low, but usually sufficient for rural demand.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:weathered basement.png| 300 px| thumb |left | Groundwater occurrence in a weathered basement aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Volcanic aquifers====&lt;br /&gt;
&lt;br /&gt;
Volcanic rocks underlie a small but significant proportion of Africa&#039;s land area, and are an important water source for tens of millions of people, many of whom live in the drought stricken areas of the Horn of Africa. Groundwater in volcanic aquifers is found within palaeosoils and fractures between lava flows. Yields can be high, and springs are important sources in highland areas.&lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:volcanic_aquifers.png| 300 px| thumb| right| Groundwater occurrence in a volcanic rock aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Consolidated sedimentary aquifers====&lt;br /&gt;
&lt;br /&gt;
Consolidated sedimentary rocks underlie around one third of Africa&#039;s land area, and can form thick, highly productive aquifers. The most significant aquifers are sandstones and limestones, which can be exploited for large urban as well as rural supplies. Mudstones however, which account for about 65% of all sedimentary rocks in Africa, contain little groundwater, and careful study is required to develop groundwater supplies from mudstones. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:sedimentary_aquifers.png| 300 px| thumb| left | Groundwater occurrence in a consolidated sedimentary aquifer]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
====Unconsolidated sedimentary aquifers====&lt;br /&gt;
&lt;br /&gt;
Unconsolidated sediments directly underlie much of Africa, and are extremely important for both rural and urban water supplies. Unconsolidated sands and gravels occur in most river valleys throughout Africa, and in many coastal areas. These deposits are often highly permeable and can store large volumes of groundwater at shallow depths, which is easy to exploit by traditional shallow wells and boreholes. &lt;br /&gt;
&lt;br /&gt;
&amp;lt;center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;div&amp;gt;&amp;lt;ul&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;li style=&amp;quot;display: inline-block;&amp;quot;&amp;gt; [[File:riverside_alluvium.png| 300 px| thumb|  right| Groundwater occurence in unconsolidated valley alluvium]] &amp;lt;/li&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/ul&amp;gt;&amp;lt;/div&amp;gt;&lt;br /&gt;
&lt;br /&gt;
&amp;lt;/center&amp;gt;&lt;br /&gt;
&lt;br /&gt;
===More Information===&lt;br /&gt;
&lt;br /&gt;
More information on geology and aquifer characteristics across Africa can be found in these [[Additional resources | resource pages]]: [[Geology | geology]]; [[Hydrogeology Map | hydrogeology map]]; and [[Aquifer properties| aquifer properties]]. More detailed information on aquifers in each country can be found in the [[Hydrogeology by country | country pages]].&lt;br /&gt;
&lt;br /&gt;
Maps summarising the hydrogeology of Africa: &lt;br /&gt;
[https://www.bgs.ac.uk/research/groundwater/international/africanGroundwater/maps.html Quantitative Groundwater Maps for Africa]&lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M. &amp;amp; Davies, J. 2000. [https://nora.nerc.ac.uk/501047/ A brief review of groundwater for rural water supply in sub-Saharan Africa]. British Geological Survey Report WC/00/033. &lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M., Bonsor, H.C., Ó Dochartaigh, B.É. &amp;amp; Taylor, R.G. 2012. [https://iopscience.iop.org/article/10.1088/1748-9326/7/2/024009;jsessionid=18D8D7F69C3ACBEED0D7494F46850BD6.c1 Quantitative maps of groundwater resources in Africa]. Environmental Research Letters 7(2). &lt;br /&gt;
&lt;br /&gt;
MacDonald, A.M. &amp;amp; Calow, R.C. 2009. [https://nora.nerc.ac.uk/8460/ Developing groundwater for secure water supplies in Africa]. Desalination 248, 546-556. doi: 10.1016/j.desal.2008.05.100&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages ]] &amp;gt;&amp;gt; Overview of Groundwater in Africa&lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Data&amp;diff=58489</id>
		<title>Groundwater Data</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Data&amp;diff=58489"/>
		<updated>2023-01-30T11:19:51Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Groundwater Data&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
This page provides an overview of groundwater data, with a particular focus on Africa; and links to further information and to available groundwater data sources.&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Groundwater Data. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
See also the [[Groundwater monitoring | &#039;&#039;&#039;Groundwater Monitoring&#039;&#039;&#039;]] page. &lt;br /&gt;
&lt;br /&gt;
You may also be interested in an [[Africa National Groundwater Databases | &#039;&#039;&#039;inventory of national groundwater databases in Africa&#039;&#039;&#039;]], and in [[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is Groundwater Data?==&lt;br /&gt;
&lt;br /&gt;
Groundwater data usually refers to &#039;&#039;&#039;measured physical or chemical information on groundwater&#039;&#039;&#039;, which is collected at points where groundwater is accessible from the surface - usually boreholes, wells or springs. &lt;br /&gt;
&lt;br /&gt;
Much useful groundwater data can be collected during drilling and testing of new boreholes. Other data must be collected from ongoing groundwater monitoring (see the [[Groundwater monitoring | &#039;&#039;&#039;groundwater monitoring&#039;&#039;&#039;]] page for more information on this). &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Examples of useful and important groundwater data that can be collected during &#039;&#039;&#039;borehole drilling and testing&#039;&#039;&#039;:&lt;br /&gt;
&lt;br /&gt;
* borehole &#039;&#039;&#039;drilling logs&#039;&#039;&#039; with geological and hydrogeological information, such as aquifer lithology, water strikes and borehole construction information.&lt;br /&gt;
* &#039;&#039;&#039;test pumping data&#039;&#039;&#039;: direct and derived data from hydrogeological tests, usually on boreholes, including pumping rates and associated drawdowns; measured aquifer properties; and estimated sustainable &#039;&#039;&#039;yields&#039;&#039;&#039;.&lt;br /&gt;
* one-off &#039;&#039;&#039;groundwater levels&#039;&#039;&#039;.&lt;br /&gt;
* one-off &#039;&#039;&#039;groundwater chemistry and microbiology&#039;&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Examples of useful and important groundwater data that must be collected by ongoing &#039;&#039;&#039;monitoring&#039;&#039;&#039; (over time):&lt;br /&gt;
&lt;br /&gt;
* &#039;&#039;&#039;groundwater levels&#039;&#039;&#039;, usually measured in boreholes or wells. These may be rest or static water levels (unaffected by groundwater pumping) or pumped water levels.&lt;br /&gt;
* &#039;&#039;&#039;groundwater chemistry and microbiology&#039;&#039;&#039;. This can include a wide range of parameters from the simple to complex: pH, alkalinity or water conductivity (SEC); inorganic chemistry including major ions such as calcium, magnesium and sodium; minor ions such as iron and manganese; or trace elements such as arsenic or cadmium; organic chemistry parameters such as nutrients and carbon or oil pollutants; microbiological parameters, often related to pathogens such as E-coli, giardia, cryptospiridium or viruses; environmental tracers including stable isotopes (such as deuterium and oxygen-18) and radioactive isotopes (such as tritium); and dissolved gases such as CFCs, methane and carbon dioxide. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
It is a challenge to collect, check, store and manage groundwater data so that it can be used effectively for groundwater development and management. Much of the information on this page relates to how and where groundwater data are stored and managed - e.g. groundwater databases - from where the data can be accessed and used. For example, an [[#Inventory of national groundwater databases in Africa  | &#039;&#039;&#039;inventory of national groundwater databases in Africa&#039;&#039;&#039;]]. &lt;br /&gt;
&lt;br /&gt;
Issues relating to collecting and checking (quality assurance or QA) groundwater data are covered here in less detail, but there are some links to further resources on these topics.&lt;br /&gt;
&lt;br /&gt;
===Who collects groundwater data?===&lt;br /&gt;
&lt;br /&gt;
Strategic groundwater data storage and management, at a national or sub-national scale, is usually the responsibility of government institutions. Data collection may be done by government agencies themselves - this is often the case for ongoing groundwater monitoring - or there may be a requirement for individuals or organisations involved in relevant activities, in particular borehole drilling, to report data to the relevant government agency. &lt;br /&gt;
&lt;br /&gt;
Groundwater data is also sometimes collected by individual research projects, for specific purposes. This data is usually limited spatially to the project area, and in time to the length of the project. It is usually not available beyond the relevant project, although in some cases, data may be shared with national government bodies and/or NGOs or other organisations involved in groundwater development and management, and/or on project websites.&lt;br /&gt;
&lt;br /&gt;
Some groundwater data are collected and stored by private organisations or NGOs, often as part of wider groundwater or water supply and management data. For example, water point mapping by NGOs working on water supply ([[#Water Point Data | Water Point Data]]), which can include some groundwater data, or data collected by mining companies or other private companies as part of their operations ([[#Groundwater Data Sources: Project-based and Private Sector | Groundwater Data Sources: Project-based and Private Sector]]).&lt;br /&gt;
&lt;br /&gt;
===How is groundwater data stored?===&lt;br /&gt;
&lt;br /&gt;
Often, groundwater data collected during drilling and testing is stored separately from groundwater monitoring data. &lt;br /&gt;
&lt;br /&gt;
Most countries have a &#039;&#039;&#039;national borehole inventory&#039;&#039;&#039; that is intended to store geological and groundwater data from the time of borehole drilling, reported by drillers and/or NGOs or other organisations active in developing water supply boreholes. These inventories can include borehole depths, drilling logs with geological information (such as lithological descriptions of the geological units drilled through), borehole construction information (such as the presence and length of borehole screens or plain casing, and whether or not the borehole has been sealed to prevent unwanted surface water inflows), and a one-off borehole water level measured during borehole drilling or immediately after construction. They may also include geophysical data from borehole siting, and test pumping data from borehole testing. &lt;br /&gt;
&lt;br /&gt;
Many countries also have one or more &#039;&#039;&#039;national groundwater (monitoring) databases&#039;&#039;&#039; intended to store ongoing (time series) data from strategic &#039;&#039;&#039;monitoring networks&#039;&#039;&#039; for &#039;&#039;&#039;groundwater level&#039;&#039;&#039; or &#039;&#039;&#039;groundwater quality&#039;&#039;&#039;. Such monitoring networks are not always fully operational, or representative of groundwater across a whole country; and monitoring data are not always easily available.&lt;br /&gt;
&lt;br /&gt;
The Atlas has compiled a [[#Inventory of national groundwater databases in Africa  | &#039;&#039;&#039;catalogue of national groundwater databases in Africa&#039;&#039;&#039;]], which provides brief details of known national borehole inventories and monitoring databases for each country in Africa. There is also a separate list below of [[#Online groundwater databases for countries in Africa | &#039;&#039;&#039;countries with online groundwater databases&#039;&#039;&#039;]]. &lt;br /&gt;
&lt;br /&gt;
==Water Point Data==&lt;br /&gt;
&lt;br /&gt;
Groundwater data is different from water point data. In recent years, the WASH sector has seen huge improvements in [https://en.wikipedia.org/wiki/Water_point_mapping  &#039;&#039;&#039;water point mapping&#039;&#039;&#039;] and, therefore, in the availability of water point data in Africa, and globally. Many new procedures, databases and digital apps have been developed - designed to allow more efficient collection, storage and availability of water point data, at project, organisation and national level, including the development of online databases. &lt;br /&gt;
&lt;br /&gt;
However, although most water points in Africa are groundwater sources, water point databases usually contain little groundwater data. Usually, therefore, they do not provide much or any information about the groundwater resource on which the water points rely. &lt;br /&gt;
&lt;br /&gt;
Some examples of data portals or digital technologies for water point data collection and management are: &lt;br /&gt;
&lt;br /&gt;
* [https://portal.mwater.co/#/ &#039;&#039;&#039;MWater&#039;&#039;&#039;] &lt;br /&gt;
* the Water Point Data Exchange ([https://www.waterpointdata.org/ &#039;&#039;&#039;WPDx&#039;&#039;&#039;])&lt;br /&gt;
* [https://akvo.org/products/akvoflow/#overview &#039;&#039;&#039;Akvo Flow&#039;&#039;&#039;]&lt;br /&gt;
* [https://www.waterpointmapper.org/ &#039;&#039;&#039;Water Point Mapper&#039;&#039;&#039;] &lt;br /&gt;
* the Sierra Leone national [https://washdata-sl.org/ &#039;&#039;&#039;WASH Data Portal&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
==An overview of groundwater data in Africa==&lt;br /&gt;
&lt;br /&gt;
The sections below provide information on key sources of groundwater data in Africa: at a [[#Groundwater Data Sources: Africa-wide or Global | continental scale]] (including global datasets that include Africa); a [[#Groundwater Data Sources: Regional within Africa | regional scale]]; a [[#Groundwater Data Sources: Country-specific / National | national scale]], including an [[#Inventory of national groundwater databases in Africa  | inventory of national groundwater databases in Africa]]; and at a [[#Groundwater Data Sources: Project-based and Private Sector | project scale or relating to private sector data]]. These data sources include groundwater source (borehole, well and spring) data and/or groundwater monitoring data.&lt;br /&gt;
&lt;br /&gt;
Groundwater monitoring is also discussed specifically on the [[Groundwater monitoring | &#039;&#039;&#039;Groundwater monitoring&#039;&#039;&#039;]] page.&lt;br /&gt;
&lt;br /&gt;
The [[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]] page describes available long term (multi-decadal) groundwater monitoring data for sites in Africa. &lt;br /&gt;
&lt;br /&gt;
===Groundwater Data Sources: Africa-wide or Global===&lt;br /&gt;
&lt;br /&gt;
====[[Long term groundwater datasets | Chronicles Consortium]]====&lt;br /&gt;
&lt;br /&gt;
The [https://www.un-igrac.org/special-project/chronicles-consortium Chronicles Consortium] initiative is collating long term - multi-decadal - records of groundwater levels from around Africa. There is a dedicated Atlas page on &lt;br /&gt;
[[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]], which provides more information on the Chronicles Consortium project and data. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:ChronConsort.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
====IGRAC [https://www.un-igrac.org/global-groundwater-information-system-ggis Global Groundwater Information System]====&lt;br /&gt;
&lt;br /&gt;
[https://www.un-igrac.org/ IGRAC] hosts the [https://www.un-igrac.org/global-groundwater-information-system-ggis &#039;&#039;&#039;Global Groundwater Information System&#039;&#039;&#039;] (GGIS) - an interactive, web-based portal to groundwater-related information. This includes some groundwater level monitoring data collated from a number of countries, including some in Africa, in the [https://ggmn.un-igrac.org/ &#039;&#039;&#039;Global Groundwater Monitoring Network&#039;&#039;&#039;] (GGMN). &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:IGRACGGIS.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
====UNHCR [https://wash.unhcr.org/wash-gis-portal/ Refugee Site Borehole Data]====&lt;br /&gt;
&lt;br /&gt;
The [https://www.unhcr.org/uk/ UNHCR] have an online [https://wash.unhcr.org/wash-gis-portal/ WASH &#039;&#039;&#039;GIS portal&#039;&#039;&#039;], which includes groundwater data from water boreholes at UNHCR refugee sites, including borehole locations, depths, casing diameters, rest (static) water levels and estimated safe yields. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:UNHCRGISPortal.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
====EAWAG [https://www.gapmaps.info/ &#039;&#039;&#039;Groundwater Assessment Platform&#039;&#039;&#039;] - groundwater quality data====&lt;br /&gt;
&lt;br /&gt;
[https://www.eawag.ch/en/ &#039;&#039;&#039;EAWAG&#039;&#039;&#039;] (the Swiss Federal Institute of Aquatic Science and Technology) developed the [https://www.gapmaps.info/ &#039;&#039;&#039;Groundwater Assessment Platform&#039;&#039;&#039;], with information on geogenic (naturally occurring in groundwater) contaminants. This database includes some measured data on groundwater arsenic and fluoride concentrations, including in Africa.   &lt;br /&gt;
{|&lt;br /&gt;
&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:EawagGAP.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Groundwater Data Sources: Regional within Africa===&lt;br /&gt;
&lt;br /&gt;
====SADC====&lt;br /&gt;
&lt;br /&gt;
An extensive report describes [https://sadc-gmi.org/wp-content/uploads/2019/07/State-of-GW-data-in-SADC_20190131.pdf the State of Groundwater Data Collection and Data Management in SADC Member States] (Sterckx et al. 2019).&lt;br /&gt;
&lt;br /&gt;
The [https://sadc-gip.org/ &#039;&#039;&#039;SADC Groundwater Information Portal&#039;&#039;&#039;] (SADC-GIP) is an online platform for sharing groundwater-related data and information in the SADC region. It includes many hydrogeological maps and databases.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===Groundwater Data Sources: Country-specific / National===&lt;br /&gt;
&lt;br /&gt;
Most countries in Africa have national groundwater data holdings, such as a water borehole inventory, a groundwater level database or a groundwater quality database. &lt;br /&gt;
&lt;br /&gt;
====Inventory of national groundwater databases in Africa====&lt;br /&gt;
&lt;br /&gt;
The Atlas has created an inventory of [[Africa National Groundwater Databases | &#039;&#039;&#039;Africa National Groundwater Databases&#039;&#039;&#039;]], which provides brief details of known national groundwater databases in Africa. &lt;br /&gt;
&lt;br /&gt;
Some of these databases are available online, and they are listed below. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:RwandaWaterPortal.JPG  | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
====Online groundwater databases for countries in Africa====&lt;br /&gt;
&lt;br /&gt;
Few countries (in Africa or elsewhere around the world) currently make such databases widely available, either in person or online, so that even where groundwater data exists at a national level, it is often not easily visible or accessible. The [[Africa National Groundwater Databases | &#039;&#039;&#039;Africa national groundwater databases inventory&#039;&#039;&#039;]] includes information on whether, and how, data from national groundwater databases are accessible. These include a growing number of countries in Africa for which some groundwater data are available online, including the following examples: &lt;br /&gt;
&lt;br /&gt;
*; Guinea Bissau&lt;br /&gt;
&lt;br /&gt;
An online [https://portal.mwater.co/#/dashboards/9c20165c8763489b85baf898bda1dca3?share=2bb0050028d540298277e50208717545 &#039;&#039;&#039;MWater Portal&#039;&#039;&#039;] allows displays data from a database storing information on nearly 1000 water boreholes, with some groundwater data including borehole depth, static water level and selected water chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Liberia&lt;br /&gt;
&lt;br /&gt;
The online [https://wash-liberia.org/ &#039;&#039;&#039;WASH Liberia&#039;&#039;&#039;] portal provides access to data from two water point surveys done in 2011 and 2017, with limited groundwater information such as water point depth, whether water is available year-round, how long it is typically dry for, if seasonally dry; and qualitative water quality information.&lt;br /&gt;
&lt;br /&gt;
*; Madagascar&lt;br /&gt;
&lt;br /&gt;
A database developed for the SADC Hydrogeological Mapping project in 2010 is available to view in the [https://sadc-gip.org/layers/geonode:gip_BHdata_madagascar &#039;&#039;&#039;SADC GMI Groundwater Information Portal&#039;&#039;&#039;], with some groundwater data, including  borehole depth, geology, aquifer type, water level, yield, and selected groundwater chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Malawi&lt;br /&gt;
&lt;br /&gt;
A database developed for the SADC Hydrogeological Mapping project in 2010 is available to view in the [https://sadc-gip.org/layers/geonode_data:geonode:BHdatabase_Malawi &#039;&#039;&#039;SADC GMI Groundwater Information Portal&#039;&#039;&#039;], with some groundwater data, including borehole depth, static water level, yield and how yield was measured, and some water chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Namibia&lt;br /&gt;
&lt;br /&gt;
The [https://www.na-mis.com/ &#039;&#039;&#039;Namibian Monitoring Information System (NA-MIS)&#039;&#039;&#039;] is an online interactive map viewer showing the locations of groundwater monitoring boreholes across Nambia and summary information on groundwater quality from monitoring boreholes. It also shows groundwater maps of Nambia: of aquifer/groundwater potential; groundwater abstraction; groundwater vulnerability; and recharge. &lt;br /&gt;
NA-MIS is available online via the [https://sadc-gmi.org/ SADC Groundwater Management Institute].&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:NA-MIS.JPG  | thumb|300px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
*; Rwanda&lt;br /&gt;
&lt;br /&gt;
The [https://waterportal.rwb.rw/ &#039;&#039;&#039;Rwanda Water Portal&#039;&#039;&#039;] allows access to groundwater level and conductivity monitoring data from a monitoring network of 24 boreholes (in 2021). Some of the groundwater level data is available to view in real time from telemetered boreholes. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:RwandaWaterPortal.JPG  | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
*; South Africa&lt;br /&gt;
&lt;br /&gt;
The South Africa Department of Water and Sanitation (DWS) has an online [https://www.dwa.gov.za/Groundwater/NGA.aspx &#039;&#039;&#039;National Groundwater Archive&#039;&#039;&#039;], which users can register for to explore groundwater related data. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:DWANGA.PNG  | thumb|300px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
*; South Sudan&lt;br /&gt;
&lt;br /&gt;
Data from a water point database collected in 2012 is available to view and download online at [https://data.humdata.org/dataset/south-sudan-water-sanitation-hygiene &#039;&#039;&#039;HDX - South Sudan Waterpoints&#039;&#039;&#039;], including groundwater data such as water point type, depth, static water level, and estimated yield. &lt;br /&gt;
&lt;br /&gt;
*; Zimbabwe&lt;br /&gt;
&lt;br /&gt;
Data from a database storing information on thousands of boreholes is available to view online in the [https://sadc-gip.org/layers/geonode_data:geonode:BHdatabase_Zimbabwe &#039;&#039;&#039;SADC-GIP Groundwater Information Portal&#039;&#039;&#039;], including groundwater data such as borehole depth, geology, aquifer type &amp;amp; potential, static water level, yield &amp;amp; how yield was measured, and selected water quality parameters.&lt;br /&gt;
&lt;br /&gt;
===Groundwater Data Sources: Project-based and Private Sector===&lt;br /&gt;
&lt;br /&gt;
Many projects and private industries carry out some form of groundwater data collection and/or monitoring. These data are often detailed, but usually focus on small areas and sometimes for short time scales (e.g. weeks to months, or in some cases a few years). These data holdings are rarely integrated with national, government-held databases. It can be difficult  for people outside the project or private company to identify what data holdings exist, and if identified, to access the data.&lt;br /&gt;
&lt;br /&gt;
An example of private sector groundwater data is groundwater level monitoring data for a shallow aquifer at a large mine in Kwale country, Kenya, which is collected by the mine operator Base Titanium. This data was shared by the mine operator with the [https://upgro.org/ UPGro] research project [https://upgro.org/consortium/gro-for-good/ Gro for Good], illustrated by a poster by [https://www.water.ox.ac.uk/wp-content/uploads/2014/10/IAH-Poster-Presentation.pdf Mutua et al (2014)]. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:MutuaetalPosterClip.PNG  | thumb|500px | Poster by [https://www.water.ox.ac.uk/wp-content/uploads/2014/10/IAH-Poster-Presentation.pdf Mutua et al (2014)] ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
An example of project-based groundwater level monitoring comes from a WaterAid project in Burkina Faso, where WaterAid initiated community-based water resource monitoring. More information is in this [[Case Study Community Monitoring Burkina Faso | &#039;&#039;&#039;case study on community monitoring in Burkina Faso&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:DippingHandDugWellBF.jpg  | thumb|300px | Dipping the water level in a hand dug well. Image credit: Djibril Barry / WaterAid (2016) ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Adelana SMA. 2009. [https://www.researchgate.net/publication/265687126_Monitoring_groundwater_use_in_Sub-Saharan_Africa_Issues_and_Challenges Monitoring groundwater resources in Sub-Saharan Africa: issues and challenges]. Groundwater and Climate in Africa: Proceedings of the Kampala Conference, June 2008, IAHS Publ. 334.&lt;br /&gt;
&lt;br /&gt;
IGRAC. 2020. [https://www.un-igrac.org/resource/national-groundwater-monitoring-programmes-global-overview-quantitative-groundwater Groundwater monitoring programmes: A global overview of quantitative groundwater monitoring networks] &lt;br /&gt;
&lt;br /&gt;
Sterckx A, Nijsten G-J, Gomo M, Lukas E and Kukurić N. 2019. [https://sadc-gmi.org/wp-content/uploads/2019/07/State-of-GW-data-in-SADC_20190131.pdf State of Groundwater Data Collection and Data Management in SADC Member States: Final report]. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &lt;br /&gt;
&lt;br /&gt;
[[Category:Groundwater data]]&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=File:Chroniclesposter.JPG&amp;diff=58488</id>
		<title>File:Chroniclesposter.JPG</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=File:Chroniclesposter.JPG&amp;diff=58488"/>
		<updated>2023-01-30T10:23:51Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Long_term_groundwater_datasets&amp;diff=58487</id>
		<title>Long term groundwater datasets</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Long_term_groundwater_datasets&amp;diff=58487"/>
		<updated>2023-01-30T10:23:35Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Long term groundwater datasets&lt;br /&gt;
&lt;br /&gt;
==The Chronicles Consortium==&lt;br /&gt;
&lt;br /&gt;
The [https://www.un-igrac.org/special-project/chronicles-consortium Chronicles Consortium] is an international consortium of scientists from across Africa and beyond, who are collating and analysing multidecadal records of groundwater levels. These datasets represent long-term aquifer dynamics, and are vital in order to assess the impacts of groundwater use, climate variability and change, and land use change on groundwater storage across Africa. The Consortium was established at the 41st Congress of the IAH (International Association of Hydrogeologists) in Marrakech, Morocco on 14 September 2014 and  led by Tamiru Abiye (Wits University, South Africa), Guillaume Favreau (IRD, France), and Richard Taylor (University College London, UK).&lt;br /&gt;
&lt;br /&gt;
The project &#039;&#039;&#039;Collation and analysis of multidecadal groundwater levels – observations in Africa&#039;&#039;&#039; was a joint initiative of the African Groundwater Network (AGW-Net), IAH Commission on Groundwater and Climate Change, and the UNESCO-IHP GRAPHIC programme, and was supported by the [https://upgro.org/ &#039;&#039;&#039;UPGro&#039;&#039;&#039;] (Unlocking the Potential of Groundwater for the Poor) programme of the UK government (DFID, NERC, ESRC) and the LMI-PICASSEAU programme of the French government (IRD). The Consortium worked with national experts in nine countries in sub-Saharan Africa, to uncover and assemble multi-decadal records of groundwater levels. The collated data were subject to rigorous analysis and were reported on in Cuthbert et al. (2019). &lt;br /&gt;
&lt;br /&gt;
The collated [https://www.un-igrac.org/chronicles-long-term-groundwater-level-anomalies-across-sub-saharan-africa &#039;&#039;&#039;Chronicles long term groundwater data&#039;&#039;&#039; ] can be downloaded from [https://www.un-igrac.org/ IGRAC]. &lt;br /&gt;
&lt;br /&gt;
More information can be seen at the [https://www.un-igrac.org/special-project/chronicles-consortium &#039;&#039;&#039;Chronicles Consortium&#039;&#039;&#039;] site.&lt;br /&gt;
&lt;br /&gt;
If you have or know of any more long term groundwater data in Africa, please contact the Consortium on chronicles@un-igrac.org  &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:chroniclesposter.JPG | thumb|400px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Cuthbert MO, Taylor RG et al. 2019. [https://doi.org/10.1038/s41586-019-1441-7 Observed controls on resilience of groundwater to climate variability in sub-Saharan Africa]. Nature 572, 230–234.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Long_term_groundwater_datasets&amp;diff=58486</id>
		<title>Long term groundwater datasets</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Long_term_groundwater_datasets&amp;diff=58486"/>
		<updated>2023-01-30T10:21:04Z</updated>

		<summary type="html">&lt;p&gt;Beod: /* The Chronicles Consortium */&lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Long term groundwater datasets&lt;br /&gt;
&lt;br /&gt;
==The Chronicles Consortium==&lt;br /&gt;
&lt;br /&gt;
The [https://www.un-igrac.org/special-project/chronicles-consortium Chronicles Consortium] is an international consortium of scientists from across Africa and beyond, who are collating and analysing multidecadal records of groundwater levels. These datasets represent long-term aquifer dynamics, and are vital in order to assess the impacts of groundwater use, climate variability and change, and land use change on groundwater storage across Africa. &lt;br /&gt;
&lt;br /&gt;
The project &#039;&#039;&#039;Collation and analysis of multidecadal groundwater levels – observations in Africa&#039;&#039;&#039; was a joint initiative of the African Groundwater Network (AGW-Net), IAH Commission on Groundwater and Climate Change, and the UNESCO-IHP GRAPHIC programme, and was supported by the [https://upgro.org/ &#039;&#039;&#039;UPGro&#039;&#039;&#039;] (Unlocking the Potential of Groundwater for the Poor) programme of the UK government (DFID, NERC, ESRC) and the LMI-PICASSEAU programme of the French government (IRD). &lt;br /&gt;
&lt;br /&gt;
The Consortium was established at the 41st Congress of the IAH (International Association of Hydrogeologists) in Marrakech, Morocco on 14 September 2014 and  led by Tamiru Abiye (Wits University, South Africa), Guillaume Favreau (IRD, France), and Richard Taylor (University College London, UK).&lt;br /&gt;
&lt;br /&gt;
The Consortium worked with national experts in nine countries in sub-Saharan Africa, to uncover and assemble multi-decadal records of groundwater levels. The collated data were subject to rigorous analysis and were reported on in Cuthbert et al. (2019). &lt;br /&gt;
&lt;br /&gt;
The collated [https://www.un-igrac.org/chronicles-long-term-groundwater-level-anomalies-across-sub-saharan-africa &#039;&#039;&#039;Chronicles long term groundwater data&#039;&#039;&#039; ] can be downloaded from [https://www.un-igrac.org/ IGRAC]. &lt;br /&gt;
&lt;br /&gt;
More information can be found at the [https://www.un-igrac.org/special-project/chronicles-consortium Chronicles Consortium] site.&lt;br /&gt;
&lt;br /&gt;
If you have or know of any more long term groundwater data in Africa, please contact the Consortium on chronicles@un-igrac.org  &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==References==&lt;br /&gt;
&lt;br /&gt;
Cuthbert MO, Taylor RG et al. 2019. [https://doi.org/10.1038/s41586-019-1441-7 Observed controls on resilience of groundwater to climate variability in sub-Saharan Africa]. Nature 572, 230–234.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &lt;br /&gt;
&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
	<entry>
		<id>http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Data&amp;diff=58485</id>
		<title>Groundwater Data</title>
		<link rel="alternate" type="text/html" href="http://earthwise.bgs.ac.uk/index.php?title=Groundwater_Data&amp;diff=58485"/>
		<updated>2023-01-30T10:12:30Z</updated>

		<summary type="html">&lt;p&gt;Beod: &lt;/p&gt;
&lt;hr /&gt;
&lt;div&gt;[[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &amp;gt;&amp;gt; Groundwater Data&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
This page provides an overview of groundwater data, with a particular focus on Africa; and links to further information and to available groundwater data sources.&lt;br /&gt;
&lt;br /&gt;
  This page is still being developed. Please check back soon for more information.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Please cite page as: Africa Groundwater Atlas. 2023. Groundwater Data. British Geological Survey. Accessed [date you accessed the information]. &#039;&#039;Weblink&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
See also the [[Groundwater monitoring | &#039;&#039;&#039;Groundwater Monitoring&#039;&#039;&#039;]] page. &lt;br /&gt;
&lt;br /&gt;
You may also be interested in an [[Africa National Groundwater Databases | &#039;&#039;&#039;inventory of national groundwater databases in Africa&#039;&#039;&#039;]], and in [[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==What is Groundwater Data?==&lt;br /&gt;
&lt;br /&gt;
Groundwater data usually refers to &#039;&#039;&#039;measured physical or chemical information on groundwater&#039;&#039;&#039;, which is collected at points where groundwater is accessible from the surface - usually boreholes, wells or springs. &lt;br /&gt;
&lt;br /&gt;
Much useful groundwater data can be collected during drilling and testing of new boreholes. Other data must be collected from ongoing groundwater monitoring (see the [[Groundwater monitoring | &#039;&#039;&#039;groundwater monitoring&#039;&#039;&#039;]] page for more information on this). &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Examples of useful and important groundwater data that can be collected during &#039;&#039;&#039;borehole drilling and testing&#039;&#039;&#039;:&lt;br /&gt;
&lt;br /&gt;
* borehole &#039;&#039;&#039;drilling logs&#039;&#039;&#039; with geological and hydrogeological information, such as aquifer lithology, water strikes and borehole construction information.&lt;br /&gt;
* &#039;&#039;&#039;test pumping data&#039;&#039;&#039;: direct and derived data from hydrogeological tests, usually on boreholes, including pumping rates and associated drawdowns; measured aquifer properties; and estimated sustainable &#039;&#039;&#039;yields&#039;&#039;&#039;.&lt;br /&gt;
* one-off &#039;&#039;&#039;groundwater levels&#039;&#039;&#039;.&lt;br /&gt;
* one-off &#039;&#039;&#039;groundwater chemistry and microbiology&#039;&#039;&#039;.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Examples of useful and important groundwater data that must be collected by ongoing &#039;&#039;&#039;monitoring&#039;&#039;&#039; (over time):&lt;br /&gt;
&lt;br /&gt;
* &#039;&#039;&#039;groundwater levels&#039;&#039;&#039;, usually measured in boreholes or wells. These may be rest or static water levels (unaffected by groundwater pumping) or pumped water levels.&lt;br /&gt;
* &#039;&#039;&#039;groundwater chemistry and microbiology&#039;&#039;&#039;. This can include a wide range of parameters from the simple to complex: pH, alkalinity or water conductivity (SEC); inorganic chemistry including major ions such as calcium, magnesium and sodium; minor ions such as iron and manganese; or trace elements such as arsenic or cadmium; organic chemistry parameters such as nutrients and carbon or oil pollutants; microbiological parameters, often related to pathogens such as E-coli, giardia, cryptospiridium or viruses; environmental tracers including stable isotopes (such as deuterium and oxygen-18) and radioactive isotopes (such as tritium); and dissolved gases such as CFCs, methane and carbon dioxide. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
It is a challenge to collect, check, store and manage groundwater data so that it can be used effectively for groundwater development and management. Much of the information on this page relates to how and where groundwater data are stored and managed - e.g. groundwater databases - from where the data can be accessed and used. For example, an [[#Inventory of national groundwater databases in Africa  | &#039;&#039;&#039;inventory of national groundwater databases in Africa&#039;&#039;&#039;]]. &lt;br /&gt;
&lt;br /&gt;
Issues relating to collecting and checking (quality assurance or QA) groundwater data are covered here in less detail, but there are some links to further resources on these topics.&lt;br /&gt;
&lt;br /&gt;
===Who collects groundwater data?===&lt;br /&gt;
&lt;br /&gt;
Strategic groundwater data storage and management, at a national or sub-national scale, is usually the responsibility of government institutions. Data collection may be done by government agencies themselves - this is often the case for ongoing groundwater monitoring - or there may be a requirement for individuals or organisations involved in relevant activities, in particular borehole drilling, to report data to the relevant government agency. &lt;br /&gt;
&lt;br /&gt;
Groundwater data is also sometimes collected by individual research projects, for specific purposes. This data is usually limited spatially to the project area, and in time to the length of the project. It is usually not available beyond the relevant project, although in some cases, data may be shared with national government bodies and/or NGOs or other organisations involved in groundwater development and management, and/or on project websites.&lt;br /&gt;
&lt;br /&gt;
Some groundwater data are collected and stored by private organisations or NGOs, often as part of wider groundwater or water supply and management data. For example, water point mapping by NGOs working on water supply ([[#Water Point Data | Water Point Data]]), which can include some groundwater data, or data collected by mining companies or other private companies as part of their operations ([[#Groundwater Data Sources: Project-based and Private Sector | Groundwater Data Sources: Project-based and Private Sector]]).&lt;br /&gt;
&lt;br /&gt;
===How is groundwater data stored?===&lt;br /&gt;
&lt;br /&gt;
Often, groundwater data collected during drilling and testing is stored separately from groundwater monitoring data. &lt;br /&gt;
&lt;br /&gt;
Most countries have a &#039;&#039;&#039;national borehole inventory&#039;&#039;&#039; that is intended to store geological and groundwater data from the time of borehole drilling, reported by drillers and/or NGOs or other organisations active in developing water supply boreholes. These inventories can include borehole depths, drilling logs with geological information (such as lithological descriptions of the geological units drilled through), borehole construction information (such as the presence and length of borehole screens or plain casing, and whether or not the borehole has been sealed to prevent unwanted surface water inflows), and a one-off borehole water level measured during borehole drilling or immediately after construction. They may also include geophysical data from borehole siting, and test pumping data from borehole testing. &lt;br /&gt;
&lt;br /&gt;
Many countries also have one or more &#039;&#039;&#039;national groundwater (monitoring) databases&#039;&#039;&#039; intended to store ongoing (time series) data from strategic &#039;&#039;&#039;monitoring networks&#039;&#039;&#039; for &#039;&#039;&#039;groundwater level&#039;&#039;&#039; or &#039;&#039;&#039;groundwater quality&#039;&#039;&#039;. Such monitoring networks are not always fully operational, or representative of groundwater across a whole country; and monitoring data are not always easily available.&lt;br /&gt;
&lt;br /&gt;
The Atlas has compiled a [[#Inventory of national groundwater databases in Africa  | &#039;&#039;&#039;catalogue of national groundwater databases in Africa&#039;&#039;&#039;]], which provides brief details of known national borehole inventories and monitoring databases for each country in Africa. There is also a separate list below of [[#Online groundwater databases for countries in Africa | &#039;&#039;&#039;countries with online groundwater databases&#039;&#039;&#039;]]. &lt;br /&gt;
&lt;br /&gt;
==Water Point Data==&lt;br /&gt;
&lt;br /&gt;
Groundwater data is different from water point data. In recent years, the WASH sector has seen huge improvements in [https://en.wikipedia.org/wiki/Water_point_mapping  &#039;&#039;&#039;water point mapping&#039;&#039;&#039;] and, therefore, in the availability of water point data in Africa, and globally. Many new procedures, databases and digital apps have been developed - designed to allow more efficient collection, storage and availability of water point data, at project, organisation and national level, including the development of online databases. &lt;br /&gt;
&lt;br /&gt;
However, although most water points in Africa are groundwater sources, water point databases usually contain little groundwater data. Usually, therefore, they do not provide much or any information about the groundwater resource on which the water points rely. &lt;br /&gt;
&lt;br /&gt;
Some examples of data portals or digital technologies for water point data collection and management are: &lt;br /&gt;
&lt;br /&gt;
* [https://portal.mwater.co/#/ &#039;&#039;&#039;MWater&#039;&#039;&#039;] &lt;br /&gt;
* the Water Point Data Exchange ([https://www.waterpointdata.org/ &#039;&#039;&#039;WPDx&#039;&#039;&#039;])&lt;br /&gt;
* [https://akvo.org/products/akvoflow/#overview &#039;&#039;&#039;Akvo Flow&#039;&#039;&#039;]&lt;br /&gt;
* [https://www.waterpointmapper.org/ &#039;&#039;&#039;Water Point Mapper&#039;&#039;&#039;] &lt;br /&gt;
* the Sierra Leone national [https://washdata-sl.org/ &#039;&#039;&#039;WASH Data Portal&#039;&#039;&#039;]&lt;br /&gt;
&lt;br /&gt;
==An overview of groundwater data in Africa==&lt;br /&gt;
&lt;br /&gt;
The sections below provide information on key sources of groundwater data in Africa: at a [[#Groundwater Data Sources: Africa-wide or Global | continental scale]] (including global datasets that include Africa); a [[#Groundwater Data Sources: Regional within Africa | regional scale]]; a [[#Groundwater Data Sources: Country-specific / National | national scale]], including an [[#Inventory of national groundwater databases in Africa  | inventory of national groundwater databases in Africa]]; and at a [[#Groundwater Data Sources: Project-based and Private Sector | project scale or relating to private sector data]]. These data sources include groundwater source (borehole, well and spring) data and/or groundwater monitoring data.&lt;br /&gt;
&lt;br /&gt;
Groundwater monitoring is also discussed specifically on the [[Groundwater monitoring | &#039;&#039;&#039;Groundwater monitoring&#039;&#039;&#039;]] page.&lt;br /&gt;
&lt;br /&gt;
The [[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]] page describes available long term (multi-decadal) groundwater monitoring data for sites in Africa. &lt;br /&gt;
&lt;br /&gt;
==Groundwater Data Sources: Africa-wide or Global==&lt;br /&gt;
&lt;br /&gt;
===[[Long term groundwater datasets | Chronicles Consortium]]=== &lt;br /&gt;
&lt;br /&gt;
The [https://www.un-igrac.org/special-project/chronicles-consortium Chronicles Consortium] initiative is collating long term - multi-decadal - records of groundwater levels from around Africa. There is a dedicated Atlas page on &lt;br /&gt;
[[Long term groundwater datasets | &#039;&#039;&#039;long term groundwater datasets in Africa&#039;&#039;&#039;]], which provides more information on the Chronicles Consortium project and data. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
| [[File:ChronConsort.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===IGRAC [https://www.un-igrac.org/global-groundwater-information-system-ggis Global Groundwater Information System]===&lt;br /&gt;
&lt;br /&gt;
[https://www.un-igrac.org/ IGRAC] hosts the [https://www.un-igrac.org/global-groundwater-information-system-ggis &#039;&#039;&#039;Global Groundwater Information System&#039;&#039;&#039;] (GGIS) - an interactive, web-based portal to groundwater-related information. This includes some groundwater level monitoring data collated from a number of countries, including some in Africa, in the [https://ggmn.un-igrac.org/ &#039;&#039;&#039;Global Groundwater Monitoring Network&#039;&#039;&#039;] (GGMN). &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:IGRACGGIS.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
===UNHCR [https://wash.unhcr.org/wash-gis-portal/ Refugee Site Borehole Data]===&lt;br /&gt;
&lt;br /&gt;
The [https://www.unhcr.org/uk/ UNHCR] have an online [https://wash.unhcr.org/wash-gis-portal/ WASH &#039;&#039;&#039;GIS portal&#039;&#039;&#039;], which includes groundwater data from water boreholes at UNHCR refugee sites, including borehole locations, depths, casing diameters, rest (static) water levels and estimated safe yields. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:UNHCRGISPortal.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===EAWAG [https://www.gapmaps.info/ &#039;&#039;&#039;Groundwater Assessment Platform&#039;&#039;&#039;] - groundwater quality data===&lt;br /&gt;
&lt;br /&gt;
[https://www.eawag.ch/en/ &#039;&#039;&#039;EAWAG&#039;&#039;&#039;] (the Swiss Federal Institute of Aquatic Science and Technology) developed the [https://www.gapmaps.info/ &#039;&#039;&#039;Groundwater Assessment Platform&#039;&#039;&#039;], with information on geogenic (naturally occurring in groundwater) contaminants. This database includes some measured data on groundwater arsenic and fluoride concentrations, including in Africa.   &lt;br /&gt;
{|&lt;br /&gt;
&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:EawagGAP.PNG | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
==Groundwater Data Sources: Regional within Africa==&lt;br /&gt;
&lt;br /&gt;
===SADC===&lt;br /&gt;
&lt;br /&gt;
An extensive report describes [https://sadc-gmi.org/wp-content/uploads/2019/07/State-of-GW-data-in-SADC_20190131.pdf the State of Groundwater Data Collection and Data Management in SADC Member States] (Sterckx et al. 2019).&lt;br /&gt;
&lt;br /&gt;
The [https://sadc-gip.org/ &#039;&#039;&#039;SADC Groundwater Information Portal&#039;&#039;&#039;] (SADC-GIP) is an online platform for sharing groundwater-related data and information in the SADC region. It includes many hydrogeological maps and databases.&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
==Groundwater Data Sources: Country-specific / National==&lt;br /&gt;
&lt;br /&gt;
Most countries in Africa have national groundwater data holdings, such as a water borehole inventory, a groundwater level database or a groundwater quality database. &lt;br /&gt;
&lt;br /&gt;
===Inventory of national groundwater databases in Africa===&lt;br /&gt;
&lt;br /&gt;
The Atlas has created an inventory of [[Africa National Groundwater Databases | &#039;&#039;&#039;Africa National Groundwater Databases&#039;&#039;&#039;]], which provides brief details of known national groundwater databases in Africa. &lt;br /&gt;
&lt;br /&gt;
Some of these databases are available online, and they are listed below. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:RwandaWaterPortal.JPG  | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===Online groundwater databases for countries in Africa===&lt;br /&gt;
&lt;br /&gt;
Few countries (in Africa or elsewhere around the world) currently make such databases widely available, either in person or online, so that even where groundwater data exists at a national level, it is often not easily visible or accessible. The [[Africa National Groundwater Databases | &#039;&#039;&#039;Africa national groundwater databases inventory&#039;&#039;&#039;]] includes information on whether, and how, data from national groundwater databases are accessible. These include a growing number of countries in Africa for which some groundwater data are available online, including the following examples: &lt;br /&gt;
&lt;br /&gt;
*; Guinea Bissau&lt;br /&gt;
&lt;br /&gt;
An online [https://portal.mwater.co/#/dashboards/9c20165c8763489b85baf898bda1dca3?share=2bb0050028d540298277e50208717545 &#039;&#039;&#039;MWater Portal&#039;&#039;&#039;] allows displays data from a database storing information on nearly 1000 water boreholes, with some groundwater data including borehole depth, static water level and selected water chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Liberia&lt;br /&gt;
&lt;br /&gt;
The online [https://wash-liberia.org/ &#039;&#039;&#039;WASH Liberia&#039;&#039;&#039;] portal provides access to data from two water point surveys done in 2011 and 2017, with limited groundwater information such as water point depth, whether water is available year-round, how long it is typically dry for, if seasonally dry; and qualitative water quality information.&lt;br /&gt;
&lt;br /&gt;
*; Madagascar&lt;br /&gt;
&lt;br /&gt;
A database developed for the SADC Hydrogeological Mapping project in 2010 is available to view in the [https://sadc-gip.org/layers/geonode:gip_BHdata_madagascar &#039;&#039;&#039;SADC GMI Groundwater Information Portal&#039;&#039;&#039;], with some groundwater data, including  borehole depth, geology, aquifer type, water level, yield, and selected groundwater chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Malawi&lt;br /&gt;
&lt;br /&gt;
A database developed for the SADC Hydrogeological Mapping project in 2010 is available to view in the [https://sadc-gip.org/layers/geonode_data:geonode:BHdatabase_Malawi &#039;&#039;&#039;SADC GMI Groundwater Information Portal&#039;&#039;&#039;], with some groundwater data, including borehole depth, static water level, yield and how yield was measured, and some water chemistry parameters.&lt;br /&gt;
&lt;br /&gt;
*; Namibia&lt;br /&gt;
&lt;br /&gt;
The [https://www.na-mis.com/ &#039;&#039;&#039;Namibian Monitoring Information System (NA-MIS)&#039;&#039;&#039;] is an online interactive map viewer showing the locations of groundwater monitoring boreholes across Nambia and summary information on groundwater quality from monitoring boreholes. It also shows groundwater maps of Nambia: of aquifer/groundwater potential; groundwater abstraction; groundwater vulnerability; and recharge. &lt;br /&gt;
NA-MIS is available online via the [https://sadc-gmi.org/ SADC Groundwater Management Institute].&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:NA-MIS.JPG  | thumb|300px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
*; Rwanda&lt;br /&gt;
&lt;br /&gt;
The [https://waterportal.rwb.rw/ &#039;&#039;&#039;Rwanda Water Portal&#039;&#039;&#039;] allows access to groundwater level and conductivity monitoring data from a monitoring network of 24 boreholes (in 2021). Some of the groundwater level data is available to view in real time from telemetered boreholes. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:RwandaWaterPortal.JPG  | thumb|200px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
*; South Africa&lt;br /&gt;
&lt;br /&gt;
The South Africa Department of Water and Sanitation (DWS) has an online [https://www.dwa.gov.za/Groundwater/NGA.aspx &#039;&#039;&#039;National Groundwater Archive&#039;&#039;&#039;], which users can register for to explore groundwater related data. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:DWANGA.PNG  | thumb|300px ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
*; South Sudan&lt;br /&gt;
&lt;br /&gt;
Data from a water point database collected in 2012 is available to view and download online at [https://data.humdata.org/dataset/south-sudan-water-sanitation-hygiene &#039;&#039;&#039;HDX - South Sudan Waterpoints&#039;&#039;&#039;], including groundwater data such as water point type, depth, static water level, and estimated yield. &lt;br /&gt;
&lt;br /&gt;
*; Zimbabwe&lt;br /&gt;
&lt;br /&gt;
Data from a database storing information on thousands of boreholes is available to view online in the [https://sadc-gip.org/layers/geonode_data:geonode:BHdatabase_Zimbabwe &#039;&#039;&#039;SADC-GIP Groundwater Information Portal&#039;&#039;&#039;], including groundwater data such as borehole depth, geology, aquifer type &amp;amp; potential, static water level, yield &amp;amp; how yield was measured, and selected water quality parameters.&lt;br /&gt;
&lt;br /&gt;
==Groundwater Data Sources: Project-based and Private Sector==&lt;br /&gt;
&lt;br /&gt;
Many projects and private industries carry out some form of groundwater data collection and/or monitoring. These data are often detailed, but usually focus on small areas and sometimes for short time scales (e.g. weeks to months, or in some cases a few years). These data holdings are rarely integrated with national, government-held databases. It can be difficult  for people outside the project or private company to identify what data holdings exist, and if identified, to access the data.&lt;br /&gt;
&lt;br /&gt;
An example of private sector groundwater data is groundwater level monitoring data for a shallow aquifer at a large mine in Kwale country, Kenya, which is collected by the mine operator Base Titanium. This data was shared by the mine operator with the [https://upgro.org/ UPGro] research project [https://upgro.org/consortium/gro-for-good/ Gro for Good], illustrated by a poster by [https://www.water.ox.ac.uk/wp-content/uploads/2014/10/IAH-Poster-Presentation.pdf Mutua et al (2014)]. &lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:MutuaetalPosterClip.PNG  | thumb|500px | Poster by [https://www.water.ox.ac.uk/wp-content/uploads/2014/10/IAH-Poster-Presentation.pdf Mutua et al (2014)] ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
An example of project-based groundwater level monitoring comes from a WaterAid project in Burkina Faso, where WaterAid initiated community-based water resource monitoring. More information is in this [[Case Study Community Monitoring Burkina Faso | &#039;&#039;&#039;case study on community monitoring in Burkina Faso&#039;&#039;&#039;]].&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
{|&lt;br /&gt;
|-&lt;br /&gt;
|&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
| [[File:DippingHandDugWellBF.jpg  | thumb|300px | Dipping the water level in a hand dug well. Image credit: Djibril Barry / WaterAid (2016) ]]&lt;br /&gt;
|}&lt;br /&gt;
&lt;br /&gt;
===References===&lt;br /&gt;
&lt;br /&gt;
Adelana SMA. 2009. [https://www.researchgate.net/publication/265687126_Monitoring_groundwater_use_in_Sub-Saharan_Africa_Issues_and_Challenges Monitoring groundwater resources in Sub-Saharan Africa: issues and challenges]. Groundwater and Climate in Africa: Proceedings of the Kampala Conference, June 2008, IAHS Publ. 334.&lt;br /&gt;
&lt;br /&gt;
IGRAC. 2020. [https://www.un-igrac.org/resource/national-groundwater-monitoring-programmes-global-overview-quantitative-groundwater Groundwater monitoring programmes: A global overview of quantitative groundwater monitoring networks] &lt;br /&gt;
&lt;br /&gt;
Sterckx A, Nijsten G-J, Gomo M, Lukas E and Kukurić N. 2019. [https://sadc-gmi.org/wp-content/uploads/2019/07/State-of-GW-data-in-SADC_20190131.pdf State of Groundwater Data Collection and Data Management in SADC Member States: Final report]. &lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
&lt;br /&gt;
Return to [[Africa Groundwater Atlas Home | Africa Groundwater Atlas]] &amp;gt;&amp;gt; [[Additional resources | Resource pages]] &lt;br /&gt;
&lt;br /&gt;
[[Category:Groundwater data]]&lt;br /&gt;
[[Category:Additional resources]]&lt;br /&gt;
[[Category:Africa Groundwater Atlas]]&lt;/div&gt;</summary>
		<author><name>Beod</name></author>
	</entry>
</feed>