Editing Hydrogeology of Burkina Faso

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==== Sedimentary - fracture flow====
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==== Sedimentary - Fracture Flow====
 
{| class = "wikitable"
 
{| class = "wikitable"
|Named aquifers||General description||Water quantity issues||Water quality issues||Recharge
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|Named Aquifers||General Description||Water quantity issues||Water quality issues||Recharge
 
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|Proterozoic to Palaeozoic (meta)sedimentary rocks
 
|Proterozoic to Palaeozoic (meta)sedimentary rocks
||Sandstones, dolomites and limestones form generally low productivity aquifer layers, which range from 50 to 1000 m thick. Dolomitic limestones form the best aquifers (BGS, 2002). The permeability of the upper aquifer layers has sometimes been enhanced by weathering (Obuobie and Barry, 2012). In some places they can be overlain by up to 60 m of alluvium, and groundwater is often in hydraulic continuity with the unconfined upper bedrock aquifer layers, with the water table ranging from 10 m to 60 m below the ground surface. The upper aquifer layers are typically unconfined.  
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||Sandstones, dolomites and limestones form generally low productivity aquifer layers, which range from 50 to 1000 m thick. Dolomitic limestones form the best aquifers (BGS 2002). The permeability of the upper aquifer layers has sometimes been enhanced by weathering (Obuobie and Barry 2012). In some places they can be overlain by up to 60 m of alluvium, and groundwater is often in hydraulic continuity with the unconfined upper bedrock aquifer layers, with the water table ranging from 10 m to 60 m below the ground surface. The upper aquifer layers are typically unconfined.  
  
 
Lower aquifer formations can be confined if overlain by dolerite intrusions or clayey layer. In confined aquifer layers, borehole water levels are typically less than 5 m below the ground surface, and in some cases are artesian.
 
Lower aquifer formations can be confined if overlain by dolerite intrusions or clayey layer. In confined aquifer layers, borehole water levels are typically less than 5 m below the ground surface, and in some cases are artesian.
  
In the Bobo Diaoulasso area, fractured and weathered schists and dolomites form a 10-30 m thick weathered aquifer, in which average borehole yields of 0.5 to 5 m³/hour and transmissivity values of between approximately 15 and 50 m²/day have been recorded (Obuobie and Barry, 2012).  
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In the Bobo Diaoulasso area, fractured and weathered schists and dolomites form a 10-30 m thick weathered aquifer, in which average borehole yields of 0.5 to 5 m³/hour and transmissivity values of between approximately 15 and 50 m²/day have been recorded (Obuobie and Barry 2012).  
  
The Gres and Intracambrian aquifers in the Bobo Dioulasso area are thought to be particularly productive aquifers. They are thought to be around 100 m thick and to have a transmissivity of approximately 120 to 415 m²/day and a specific capacity of 1 m³/hour/m (Obuobie and Barry, 2012).  
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The Gres and Intracambrian aquifers in the Bobo Dioulasso area are thought to be particularly productive aquifers. They are thought to be around 100 m thick and to have a transmissivity of approximately 120 to 415 m²/day and a specific capacity of 1 m³/hour/m (Obuobie and Barry 2012).  
  
 
Yield data from the Burkina national borehole database indicates average borehole yields of around 4.5 m³/hour.  
 
Yield data from the Burkina national borehole database indicates average borehole yields of around 4.5 m³/hour.  
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||The aquifer is used for water supply in rural and urban areas (70% of abstraction from the aquifer); and also for mineral water and other commercial/industrial use (25%) and other uses.
 
||The aquifer is used for water supply in rural and urban areas (70% of abstraction from the aquifer); and also for mineral water and other commercial/industrial use (25%) and other uses.
 
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||Most recharge to the aquifer is thought to occur from seasonal rainfall infiltration by preferential flow through fractures (Obuobie and Barry, 2012).  
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||Most recharge to the aquifer is thought to occur from seasonal rainfall infiltration by preferential flow through fractures (Obuobie and Barry 2012).  
 
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