Hydrogeology of Ethiopia
- 1 Authors
- 2 Geographical Setting
- 3 Geology
- 4 Hydrogeology
- 5 Groundwater use and management
- 6 References
- 7 Return to the index pages
Dr Seifu Kebede, Addis Ababa University, Ethiopia
Addis Hailu, University of Gondor, Ethiopia
Emily Crane & Brighid Ó Dochartaigh, British Geological Survey, UK
Ethiopia's landscape includes a large highland area of mountains and dissected plateaus, divided by the Rift Valley, which runs generally southwest to northeast and is surrounded by lowlands, steppes, or semi-desert. This large diversity of terrain has led to wide variations in climate, soils and natural vegetation.
|Estimated Population in 2013*||94100756|
|Rural Population (% of total)*||81.41%|
|Total Surface Area*||1000000 sq km|
|Agricultural Land (% of total area)*||36.488%|
|Capital City||Addis Ababa|
|Border Countries||Eritrea, Sudan, South Sudan, Kenya, Somalia, Djibouti|
|Annual Freshwater Withdrawal (2013)*||5558 Million cubic metres|
|Annual Freshwater Withdrawal for Agriculture*||93.6%|
|Annual Freshwater Withdrawal for Domestic Use*||6.0%|
|Annual Freshwater Withdrawal for Industry*||0.4%|
|Rural Population with Access to Improved Water Source*||42.1%|
|Urban Population with Access to Improved Water Source*||96.8%|
* Source: World Bank
The highlands in the central-west of the country are temperate, with high annual rainfall, or tropical savannah, with distinct dry and wet seasons. In the lowland areas in the east, the climate is arid steppe or arid desert, and is significantly hotter and drier.
Temporal variations in temperature and rainfall.
For further detail on the climate datasets used see the climate resources section.
|The highlands of Ethiopia are the source of major perennial rivers, and Ethiopia also has a number of large lakes. Lake Tana, in the north, is the source of the Blue Nile, and there are a number of other major rivers. However, apart from these major surface water features, there are hardly any perennial surface water flows in areas below 1,500 m.
The Hydrology Directorate of the Ethiopian Ministry of Water Irrigation and Energy is the responsible body for installation and maintainence of river gauges. They also manage and disseminate the resulting river discharge data.
Most hydrological records started in the 1960s following the initiation of the Blue Nile Basin Master Plan study by the USBR (United States Bureau of Reclamation). There are currently 489 operational river gauging stations in Ethiopia.
Ethiopia is an ecologically diverse country, including deserts along the eastern border; tropical forests in the south; and extensive mountains in the north and southwest.
The following section provides a summary of the geology of Ethiopia. More detailed information can be found in the key references listed below: many of these are available through the Africa Groundwater Literature Archive.
The geology map on this page shows a simplified version of the geology of Ethiopia at a national scale (see see the Geology resources page for more details).
|Key Formations||Period||Lithology||Thickness and important structural features|
|Igneous - volcanic|
|Rift volcanics||Quaternary||Rift related, unwelded and welded pyroclastics and basalts. Composed of ash, pumice, ignimbrites and pyroclastics.||Thickness reaches 500 metres; multiple sets of faults, fractures and volcanic landforms, isolated volcanoes and cones, calderas and craters|
|Quaternary plateau basalts||Quaternary||Scoraceous basalts, mostly vesicular and scoraceous. Have a limited lateral extent.||Associated with central eruptions from volcanic centres on the plateau; mainly associated with shields.|
|Shield volcanics||Miocene (Tertiary)||Basalts intercalated with minor acid volcanic rocks (eg rhyolites) and trachytes. The basal diameters of the shields range from 50 to 100 km. They radiate from a peak, and dip at an angle of 5°.||500 metres; broad based (up to 100 km) shields dotting the Ethiopian plateau|
|Aiba, Alaji and Termaber formations (Upper Basalts)||Oligo-Miocene (Tertiary)||Basalts with intercalations of rhyolites and ignimbrites towards the top part. Can be associated with shield volcanics. Mostly massive basalt, but columnar jointed layers are common. Layers of acidic rocks, rhyolites and tuffs are also common. Paleosol layers may be visible between the contact of this unit with the the underlying Ashangie Formation.||Thickness 1000 metres. Typically forms flat topped, uniform plateau areas, with cliffs at plateau edges.|
|Ashangie Formation (Lower Basalts)||Oligocene (Tertiary)||Deeply weathered, brecciated basalts||500 metres, forms rugged terrain|
|Sedimentary - Miocene (Tertiary) to Recent|
|Alwero Formation (largely consolidated) and associated unconsolidated sediments||Miocene (Tertiary) to Recent||
||1 km?. The Basin forms part of the Blue Nile rift in South Sudan and extends toward the west|
|Sedimentary - Eocene|
|Auradu and Taleh formations - carbonate and evaporite rocks||Eocene (Tertiary)||Interbedded limestone, evaporite (anhydrite, gypsum) and shale||500 metres; karst features observed|
|Sedimentary - Upper Cretaceous|
|Jessoma Sandstone||Upper Cretaceous||Detrital, poorly cemented sandstone||500 metres; poor surface drainage and plain forming- extends south up to Mogadishu in Somalia|
|Sedimentary - Lower Cretaceous|
|Korahe Formation||Lower Cretaceous||Marine deposits; interbedded gypsum, shale, anhydrite, dolomite, limestone and sandstone||Not known|
|Sedimentary - Jurassic|
|Gabredarre, Hamanile, Urandab and Antalo formations - limestones||Jurassic||Dominantly limestone (75%) with some shale, marl and gypsum intercalations
The Gabredarre Formation includes oolitic limestones, marls and some gypsum. It is horizontally bedded and characterised by karst features, including solitary caves such as the famous Sofomar caves. The limestones of the Sofomar caves region have the highest degree of karstification of Ethiopia's carbonate rocks. The Gabredarre Formation has limestone cliffs that are moderately jointed and have intercalations of sand, marl and gypsum beds. The Gabredarre Formation grades down to the underlying Urandab Formation, which is the equivalent of the Antalo Limestone.
The Hamanile Formation consists of organogenic and oolitic limestones with shale and sandstone. The limestones are well jointed. The Haminile limestone plateau occurs on the Dolo to Negele Borena road around Bidre and consists of a marly, fractured, thinly (~1m) bedded limestone. Around Negele Borena the Hamanile limestone formation can be classified into at least five sub-units characterized by variable lithologies and intercalations. The succession is thinnest in the area of Negele town. The maximum thickness is about 700 m in the area of Filtu.
|Adigrat Sandstone||Jurassic||Highly cemented sandstone. The top part has been altered by heating from Cenozoic volcanism.||700 metres|
|Precambrian Mobile/Orogenic belt|
|Precambrian: Medium-High grade Mozambique belt in south and west Ethiopia||Proterozoic||Paleoproterozoic metasediments and gneiss and pre- and syn-tectonic granites. Generally high grade metamorphic rocks are interbedded with low grade metamorphic rocks||This part of the basement in Ethiopia, unlike the basement in much of central Africa, has undergone multiple episodes of deformation and orogenesis.|
|Precambrian: Low grade Arabian Nubian Shield in Northern Ethiopia||Proterozoic||A transition zone between low grade volcano sedimentary succession and mafic ultramafic complexes of the Arabian Nubian Shield. The key lithologies are metavolcano sedimentary rocks and post-tectonic granite intrusive igneous rocks.|
The most important aquifers in Ethiopia are formed by unconsolidated Quaternary sediments; Tertiary-Quaternary volcanic rocks; and Mesozoic consolidated sedimentary rocks. Basement aquifers are also important locally. A summary of these aquifers and their physical and chemical characteristics is in the tables below. More detailed information is available in the references listed below each table: many of these are available through the Africa Groundwater Literature Archive.
The hydrogeology map on this page shows a simplified version of the type and productivity of the main aquifers at a national scale (see the Hydrogeology Map resource page for more details).
Other hydrogeological maps from different sources have been produced and are available in different formats. Some can be viewed on the WHYMAP website.
|Named Aquifers||General Description||Water quantity issues||Water quality issues||Recharge|
|Alluvial sediments||Afar Region: alluvial deposits in floodplains have moderate to high permeability, with measured transmissivity from 1-500 m²/day and yields of up to 20 l/s. These aquifers can be unconfined and confined; they vary in thickness from 0 - 400 metres; water table depth is typically in the range 1 to 60 metres; typical borehole depth is 100 m; salinity is very variable.
In the Holocene alluvial aquifer borehole yields of 0.1 to 1 l/s have been recorded. Water levels are usually less than 5 m below ground surface.
Northern Ethiopia: alluvial sediments overlying basement rocks can store appreciable volumes of water and are characterised by high permeability and high water infiltration capacity. They are typically shallow and have limited lateral extent, and form perched aquifers. Springs and hand-dug wells are common, with recorded yields ranging between 0.05 l/s and 0.17 l/s.
|Afar Region - high productivity. Northern Ethiopia - low productivity.||Variable salinity|
|Alluvio-lacustrine sediments||These sediments have highly variable permeability. Fine sand deposits have the highest permeability, with some boreholes providing more than 10 l/s with minimal drawdown. Transmissivities range up to 700 m²/day and specific yields are of the order of 3.2 l/s/m. In several places higher transmissivities have been noted. For example, a 150 m deep borehole in alluvio-lacustrine deposits at the foot of the southern plateau has a transmissivity of 3012 m²/day. These aquifers can be both unconfined and confined; they vary in thickness from 0 to 400 metres; water table depth is typically in the range 1 to 60 metres; and the typical borehole depth is 100 m.
Fine-grained sands interbedded with massive volcanic tuffs and fine ash are known to have low productivity in many places (e.g. in the central Ethiopian Rift). In the eastern part of the country the total thickness of these sediments can reach about 300 m. In most of the outcrops, they consist of conglomerates, sandstone and mudstone, which are gypsiferous and locally bear saline groundwater.
|Can be highly productive||Variable salinity|
|Quaternary Alluvial Aquifers within Lake Tana basin||These occur dominantly in the eastern part of the basin following the lower Rib and lower margin of Gumera and Fogera plain (East of Lake Tana). They also cover a significant area of the north part of the basin at the lower part of the Megech and Western shore of Lake Tana. However, the distribution of alluvial sediments is limited compared to the volcanic aquifers. The deposits vary in thickness from 1 to 400m. The aquifers can be unconfined or confined. Water table depth is typically in the range 1 to 60 metres, and typical borehole depth is 100 m.
The productivity of this aquifer is controlled by the intergranular permeability of the unconsolidated gravels, sand and clay. They are typically high productivity aquifers, with boreholes up to 60 m depth recorded as yielding more than 6 l/s.
The previous investigation aided with drilling on the lake floor shows the occurrence of indicates stiff clay up to 80 m depth.
|Moderate to high productivity||Variable salinity|
|Wadi bed aquifers||Although localised, these intergranular aquifers have significant groundwater potential in water scarce arid and desert settings. Wadi bed length exceeds 30 000 km across Ethiopia, and total groundwater storage in these aquifers could be as much as 3 billion cubic metres. The most important wadi aquifers, which support the livelihoods of millions of people living a pastoral lifestyle, include those in Borena, Lower Omo, Ogaden, the Western Lowlands bordering Sudan, and in the Afar depression. The most productive wadi bed aquifers are those dominated by sandy and gravelly sediments with a low proportion of clay.
One of the highest yielding recorded boreholes abstracting from a wadi bed aquifer is the El-Gof borehole, which taps an intergranular sand and gravel aquifer, overlain by lacustrine sediments, and has a yield of 5 l/s. Other boreholes have recorded discharges of 0.5 l/s to 8 l/s.
|Important source of groundwater in areas with little surface water||Variable salinity|
|Talus slope, landslide bodies, alluvial terraces||These deposits form small outcrops 0.5 to 2 km² in area. Permeability is enhanced in areas where the material is loosely packed. Groundwater from mountain areas flows towards the talus slope and landslide deposits, from where springs commonly emerge. Typical spring yields are 1 to 2 l/s. These aquifers with readily available groundwater discharges support several villages in areas of relatively gentle slopes and good soil development.||Variable salinity||Recharged from groundwater flowing from higher elevation|
Key references for Quaternary unconsolidated aquifers of Ethiopia are Alemneh (1989); Chernet (1993) and Hadwen et al. (1973) (for more details see Key Hydrogeology References).
Igneous - Volcanic
|Named Aquifers||General Description||Water quantity issues||Water quality issues||Recharge|
|Rift volcanics||Generally low productivity with low borehole yields, from 1 to 5 l/s. In some conditions the aquifer is confined, leading to artesian conditions.||Low borehole yields||High fluoride and salinity, often exceeding WHO limits.||Both direct rainfall and indirect (eg from river beds) recharge is common.|
|Quaternary plateau basalts||The most extensive occurrence is in the Lake Tana Basin, where these form a highly productive, fractured aquifer, with borehole yields reaching 20 l/s (there are other records of borehole yields of between 5 and 100 l/s), and groundwater discharge to rivers and springs. Elsewhere in Ethiopia the Quaternary volcanics are highly productive but have dual fracture-intergranular porosity.||Highly productive||Good water quality: generally bicarbonate type, low salinity, low fluoride.||Direct and indirect recharge occurs.|
|Shield volcanics||This aquifer can be up to 500 m thick. Groundwater discharge occurs through springs, which are common at the foot of the shield areas. The intercalation of volcanic ash with basalt forms a dual porosity and permeability groundwater system: groundwater storage is focussed in ash layers, while groundwater flow is focussed through fractures in the basalt layers. Shield areas dominated by acid volcanic rocks show lower groundwater potential (e.g. in the Bale Massif). The aquifer is typically unconfined to semi confined. The depth to water ranges from 5 to 60 m, and borehole depths are typically 60 to 150 metres.||Good water quality: generally bicarbonate type, low salinity, low fluoride.||Recharge occurs through fractures in highland areas.|
|Upper basalt aquifer (Aiba, Alaji and Termaber formations)||This aquifer forms the most productive of the volcanic aquifers in Ethiopia. It is typically unconfined to semi-confined and often artesian. Groundwater discharge occurs to wetlands and to springs on cliffs. The aquifer thickness ranges from 50 to 1000 m. The depth to water table varies from 0 to 250 metres. Borehole depths are typically from 100 to 150 m. Borehole yields are generally up to 20 l/s.
The Aiba Formation has dual porosity, with groundwater occurring in joints, fractures and scoriaceous layers. Deep boreholes show the presence of narrow but extensive fracture zones with high permeability and low storage. Transmissivity varies between 0.5 and 1400 m²/day. Borehole yields range from 5 to 150 l/s.
Pumping test analysis and well logs from the Termaber Formation show that it is dominated by fracture flow.
|The most productive of the volcanic aquifers.||Good water quality: generally bicarbonate type, low salinity, low fluoride.||Recharge occurs vertically through the soil zone and fractures in the rocks.|
|Lower basalt aquifer (Ashangie Formation)||These rocks are characterised by rugged topography with dissected and irregular morphology. The rocks are deformed, and in their northern section dip at up to 40°. They are thinly bedded, and in several areas are brecciated. Field evidence shows that the brecciated parts are characterized by lower permeability. The rocks are typically deeply weathered, when they are reddish in colour, but generally have low permeability. Both primary (vesicle) porosity and secondary (fracture) porosity have been modified and reduced by secondary mineralisation (e.g. by calcite, zeolite and silica).
In more detail, the Ashangie Formation can be divided into three zones:
1) an upper layer, with gentle topographic slopes. Mostly scoriaceous, with several thin beds of clay soils. Recharge occurs vertically through this layer to the underlying layers. Springs are rare, and most groundwater discharge occurs as diffuse seepage on slopes, often contributing to landslides.
2) a thinner middle, more resistant layer, which often forms cliffs. When exposed at the ground surface by erosion, this can form locally extensive plateau areas, such as around the Upper Tekeze plains, Lalibela and the Belesa plain. Typically has higher groundwater productivity.
3) a lower layer, also with gentle slope. Mostly scoriaceous, with several thin beds of clay soils. Often contains cross-cutting dykes which are conduits for groundwater convergence and discharge.
The aquifer thickness varies up to 500 m. The rugged topography means that the aquifer is not laterally extensive. Depressions in the rugged terrain are areas of groundwater discharge.
The aquifer is usually unconfined to semi-confined. Typical borehole yields are between 0.5 and 20 l/s. Transmissivity ranges between 0.5 and 85 m²/day. The water table depth is typically between 100 and 200 m, and borehole depths are typically 150 to 200 m.
The contact between this unit and the upper basalt above is characterised by spring discharge.
|Good water quality: generally bicarbonate type, low salinity, low fluoride.|
Key references for volcanic aquifers of Ethiopia are Kebede (2013) and Ayenew et al. (for more details see Key Hydrogeology References).
Mesozoic Consolidated Sedimentary Aquifers with Fracture and Intergranular Flow
Notable hydrogeologic and geologic features of Mesozoic sedimentary rocks of Ethiopia are:
- Uplifting and formation of tabular plateaus;
- deep incision by river gorges;
- absence of or limited karstification in carbonate rocks;
- absence of regional folding and flexures at the margins of the units; and
- extensive cover by younger volcanic rocks.
These features contrast with typical sedimentary basins elsewhere in Northern and Eastern Africa. In contrast to the sedimentary basin aquifers of northern and Sahel Africa, structural traps (such as synclines formed by compressional deformation) are uncommon, leaving little room for large volume groundwater storage.
|Named Aquifers||General Description||Water quantity issues||Water quality issues||Recharge|
|Hamanile, Gabredarre and Antalo formations (Jurassic limestones)||The Gabredarre Formation is characterised by karst features, including caves. The limestones of the Sofomar caves region have the highest degree of karstification of Ethiopia's carbonate rocks. The aquifer has moderate permeability and productivity.
The Hamanile Formation limestones are well jointed with moderate to high permeability. Evidence from boreholes in highland and midlands areas, where the aquifer crops out, shows that groundwater levels can be very deep: for example, more than 200 m below ground level between Filtu and Negele. Where the water table is shallower, the Hamanile limestones form relatively productive aquifers.
In general, these aquifers are typically 500 to 1000 m thick, and are unconfined to semi-confined. The water table is usually 200 to 400 m deep; typical borehole depth is 300 m.
|Good quality water generally. However, high concentrations of dissolved salts, including sodium, chloride and/or sulphate, occur due to reaction with abundant minerals in evaporite beds, and salinity can reach 3 mg/l.||In high rainfall highlands, recharge could reach 200 mm/yr. In arid regions it varies between 10 mm/yr and 50 mm/yr.|
|Adigrat Formation (Jurassic sandstone)||The highly cemented Adigrat Formation has low primary porosity, and the top part has been altered by heating by Cenozoic volcanism. Fracturing has created secondary porosity and permeability. The emergence of springs at the contact of the Adigrat sandstone and the overlying volcanic rocks is indicative of the low permeability of the Adigrat Formation.
This aquifer is typically 200 to 1000 m thick and is unconfined to semi-confined. The water table is usually 200 to 400 m deep; typical borehole depth is 300 m.
|Very good quality water||In highlands areas with high rainfall, recharge could reach 200 mm/yr. In arid regions it varies between 10 mm/yr and 50 mm/yr.|
Key references for Mesozoic sedimentary aquifers of Ethiopia are BSEE (1973), Chernet (1993), Hadwen et al. (1973), Haile et al (1996) and Kebede (2013) (for more details see Key Hydrogeology References).
|Named Aquifers||General Description||Water quantity issues||Water quality issues||Recharge|
|Precambrian basement aquifers of Southern Ethiopia and Northern Ethiopia; Crystalline Basement aquifers of Western Ethiopia||
Basement aquifers in general
The productivity of basement aquifers in Ethiopia largely depends of the development of regolith (weathered rock) amd the density of fractures. In turn, these are partly controlled by the type or grade of metamorphic rock that forms the basement. Less important controls on groundwater occurrence are the sustainability of recharge; and topography. Groundwater in the basement aquifers occurs in shallow regolith (weathered rock) basins.
Borehole yields from the most productive boreholes in basement aquifers are generally less than 0.1 l/s. Spring discharges in the basement complex are of the order of 1 l/s. Generally, basement aquifers in western and south-central parts of Ethiopia are productive, and the lowest productivity basement aquifers are located in northern Ethiopia and the Borena lowlands (near the southern border).
The basement aquifers are unconfined. Aquifer (regolith) thickness varies from 0 to 60 m (thinner in northern Ethiopia and thicker in western Ethiopia - see below). The deepest known borehole struck water at 100 m. The water table is typically 2 to 60 m deep. Boreholes tend to be 60 to 120 m deep.
|Yield is very low in unweathered basement rocks and highest (~0.1 l/s) where weathering and regolith is most developed||Good quality||Recharge varies from 10 to 250 mm/yr depending on rainfall regime|
The key reference for basement aquifers of Ethiopia is Kebede (2013) (for more details see Key Hydrogeology References).
Recharge over Ethiopia is extremely variable. It varies from nearly 0 to 300 mm/yr. Nearly 60% of aquifers receive indirect recharge from floods, mountain runoff, as well as fast recharge from high rainfall events. Diffuse recharge is limited to the plateau region which accounts for around 30% of the country.
The geological uplift in the Cenozoic which led to erosion and dissection of the aquifers into smaller size units, has resulted in generally low storage compared to large sedimentary basins elsewhere in Africa. The storage to recharge ratio is around 28 years (Kebede, 2013).
Groundwater quality is highly variable across Ethiopia, from fresh waters in many of the springs flowing from basement aquifers, to more saline waters in volcanic aquifers in parts of the Rift Valley and sedimentary aquifers of the plains. Key issues are high fluoride concentrations and/or total dissolved salts in volcanic aquifers in the Rift Valley, linked to the influence of geothermal waters; and increased salinity in many groundwaters in sedimentary aquifers in the south, southeast and northeast of the country, linked to the dissolution of evaporite minerals.
Key references for more information on groundwater quality in Ethiopia are:
British Geological Survey/WaterAid. 2001. Groundwater Quality: Ethiopia. Leaflet.
- Groundwater quantity
Annual renewable groundwater resources stands around 36 Billion meter cube. Storage varies between 1000 to 10000 billion m³.
- Groundwater guality
Nearly 30% of groundwater storage is not available for direct use because of high salinity and/or high fluoride.
- Groundwater-Surface Water Interaction
- There are a number of groundwater dependent surface waters, including wetlands and lakes. - Wetlands are increasingly threatened by deepening, widening and propagating gullies as well as by infestation by invasive weeds
- Groundwater Dependent Ecosystems
There is low recognition at government level of the fact that wetlands are groundwater dependent.
Groundwater use and management
Some 80% of the total national water supply comes from groundwater.
Groundwater provides most of the water for domestic supply (90%) and industrial use (95%), but only a very small proportion of irrigation demand (<1%). Groundwater use for livestock watering is unknown.
Kebede (2013) gives national estimates of groundwater abstraction volumes.
Groundwater sources in Ethiopia consist of:
- Hand dug wells
- Improved cold springs
- River bed excavations/pits
- Traditional Ella wells (very large diameter wells)
There are currently no regional or national groundwater level or quality monitoring programmes.
The key groundwater institutions, and their roles, are:
- Ministry of Water Irrigation and Energy- Regulatory, policy, financing, planning, maintenance of information base
- Geological Survey of Ethiopia- Exploration and Mapping
- Ministry of Forestry and Environment: Reviewing possible impacts of national investments on groundwater quality and quantity; Selected strategic environmental assessments – linked to groundwater management plans
- Agricultural Transformation Agency- Shallow groundwater mapping and management policy
- Regional Water Bureaus- Regulatory, policy, financing and planning
- Water Works Enterprises- Study, Design, Supervision and Development
- Regional Ministry of Forestry and Environment: Licensing and Impact assessment of investment on groundwater
- River Basin Organizations: Allocation and supplies
- Water User Associations: Local regulation and allocation
- Technical and vocational Schools (TVETs): training human power in groundwater development , low skill
There is a limited legal framework for groundwater management, but the regulations are not systematically implemented. No regulatory provision exists to protect vulnerable areas. The report “Groundwater Management framework document (MWR, 2010)” includes the following regulatory provisions:
- No person shall be engaged in the drilling or rehabilitating of water wells without a permit duly issued by the Ministry or his designee.
- Any person who wants to have water well drilled shall first acquire a permit to do so from the Ministry or his designee before entering a contract for this purpose with a water well drilling or rehabilitating contractor. Applications made to have a water well drilling or rehabilitating contractor. Applications made to have water well drilled must be accompanied with the design and specifications of such well.
- All water well drillers and rehabilitators shall, before entering in to a contract to drill water well, first ensure that the Ministry or his designee has approved that such well be drilled.
- All persons who want to have a water well drilled or rehabilitated shall, before entering in to a contract to have such water well drilled or rehabilitated, first ensure that the driller or rehabilitator has a permit to undertake the drilling or rehabilitating or water wells.
- A well driller or rehabilitator shall, within three months of completing a well drilling or rehabilitation, submit to the Ministry or his designee a technical report – that includes information about the drilling, construction and rehabilitation process, the geological and electrical log, yield tests, laboratory tests, problems encountered during drilling, construction and rehabilitation, pump installed.
The major transboundary aquifers in Ethiopia are:
- The unconsolidated sedimentary aquifers of Gambella (Upper Blue Nile) and Alwero Sandstone: Ethiopia and South Sudan
- The Bulal Basalt aquifer: Ethiopia and Kenya
- The Hanle Graben aquifer: Djibouti and Ethiopia
- The Sedimentary Basin of Ogaden: Ethiopia and Somalia
No management system exists specifically pertaining to transboundary aquifers. Conflict over water sources in general is common among pastoralists in the border region of Ethiopia and Kenya.
Many of the references below, and others relating to the hydrogeology of Ethiopia, can be accessed throughthe African Groundwater Literature Archive.
Geology: key references
Beyth M. 1972. The Geology of Central Western Tigre, Ethiopia. University of Bonn, p. 155.
EGS. 1996. Geological map of Ethiopia at 1:2000000 scale. Ethiopian Geological Survey, Addis Ababa, Ethiopia
Davidson A. 1983. The Omo River Project. Reconnaissance geology and geochemistry of parts of Illubabor, Kefa, Gemu Gofa and Sidamo, Ethiopia. Ethiopian Institute of Geological Surveys Bull 2, 89 pp.
Kazmin V, Shiferaw A and Balcha T. 1978. The Ethiopian basement: stratigraphy and possible manner of evolution. GeologischeRundschau 67, 531–548.
Kieffer B, Arndt N, Lapierre H et al. 2004. Flood and Shield Basalts from Ethiopia: Magmas from the African Superswell. J of Petrology 45:793-834
Le Turdu C, Tiercelin JJ, Gibert E et al. 1999. The Ziway–Shala lake basin system, Main Ethiopian Rift: influence of volcanism, tectonics, and climatic forcing on basin formation and sedimentation. Palaeogeography, Palaeclimatology and Palaeoecology 150: 135–177.
Mohr P. 1973. Crustal deformation rate and the evolution of the Ethiopian rift. In: Tarling DH, Runcorn SK (eds) Implications of continental drift to the earth sciences. Academic Press, London, pp 767–776
Mohr P. 1983. Ethiopian Flood Basalt Province. Nature 303:577- 584.
Mohr P and Zanettin B. 1988. The Ethiopian flood basalt province. In: Macdougall, J. D. (ed.) Continental Flood Basalts. Dordrecht: Kluwer Academic, pp. 63---110.
Rochette P, Tamrat E, Feraud G et al. 1998. Magnetostratigraphy and timing of the Oligocene Ethiopian Traps. Earth and Planet.Sci. Lett, 164: 497-510.
Taddesse T, Hoshino M, Sawada Y. 1999. Geochemistry of low-grade metavolcanic rocks from the Pan-African of the Axum area, northern Ethiopia. Precambrian Research 99: 101–124
USBR. 1964. Land and water resources of the Blue Nile basin, Ethiopia. United States Bureau of Reclamation, Main report, Washington.
WoldeGabriel G, Walter RC, Aronson JL. 1992. Geochronology and distribution of silicic volcanic rocks of Plio-Pleistocene age from the central sector of the Main Ethiopian Rift. Quat. Int. 13–14, 69–76.
Zanettin B, Justin-Visentin E. 1974. The volcanic succession in central Ethiopia, the volcanics of the western Afar and Ethiopian Rift margins. Univ. Padova Inst. Geol. Mineral. Mem. 31, 1–19.
Hydrogeology: key references
Alemneh S. 1989. Hydrogeology of Yabello sheet (NB37-14). Ethiopian Geological Survey report number 307. Addis Ababa, 40pp.
Ayenew T, Demli M and Wohnlich S. DATE. Occurrence of groundwater in Ethiopian volcanic terrain. Journal of Africa Earth Sciences, 52 (3), 97–113.
BCEOM. 1999. Abay River Basin integrated master plan, main report, Ministry of Water Resources, Addis Ababa.
Belete Y, Alemirew D, Mekonen A et al (2004) Explanatory notes to the hydrogeological and hydrochemical maps of the Asosa-Kurmuk Area (NC36-7 West of Assosa and NC36-8 Assosa sheets), Geological Survey of Ethiopia, Addis Ababa, 120 pp.
BSEE. 1973. The caves of Ethiopia, The 1972 British SpeleologiclaExpediation to Ethiopia. Transaction Cave Research Group of Great Britain, 15:107-168
Chernet T. 1982. Hydrogeologic map of the lakes region (with memo) Ethiopian Institute of Geological Survey (now Ethiopian Geological Survey), Addis Ababa Ethiopia.
Chernet T. 1993. Hydrogeology of Ethiopia and water resources development Ethiopian Institute of Geological Surveys, Addis Ababa, 222pp.
Gasse F. 1977. Evolution of Lake Abhe (Ethiopia and TFAI), from 70,000 BP. Nature (London) 265 (5589), 42– 45.
Gasse F, Street FA. 1978. Late Quaternary lake level fluctuations and environments of the northern Rift Valley and Afar region (Ethiopia and Djibouti)- Paleogeogr. Paleoclimatol. Paeoecolo.24: 279-221
Hadwen P. 1975. Boreholes in Ethiopia. Geological Survey of Ethiopia, Unpublished report number 29, Hydrogeology Division, Technical Memorandum 9, Addis Ababa, 22pp.
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