^{1}

^{2}

Genale-Dawa River Basin is one of the largest and most drought prone re-gions in Ethiopia. As a result a search for alternative source of water has always been a major issue in the region. This study therefore, aims at characterizing and evaluating the ground water potential resource of the river basin. The delineation and numerical discretization of the river basin were primarily done for the proper development of the problem domain. And the groundwater governing equation was solved at individual nodal points of the discretized region using a 3-D numerical ground water model called TAGSAC. This resulted in monthly average groundwater table fluctuation and replenishable ground water potential estimation. Hydrogeological classification was also done based on hydraulic conductivity values obtained from model calibration.

Ethiopia, being one of the most hydrologically blessed countries in east Africa, is believed to have a large ground water potential reserve. Studies show erroneous results of 2.5 BCM by WAPCOS, to 185 BCM by Ayenew and Alemayehu, in 2001 [

The country’s water supply coverage was estimated to be 30.9 percent, the rural water supply coverage being 23.1 percent and that of urban being 74.4 percent [

Ethiopia has suffered from repeated drought scenarios in the past; especially the peripheries of the country like Genale-Dawa basin are more prone to drought than the interior highlands. At driest seasons even major surface water sources dry up; as a result the available large areas of suitable irrigation land are left uncultivated and in times; standard domestic water supply become scarce. As a result proper management and utilization of water resource is vital in the region. In the past, studies have been done on the region to estimate the water resource potential. However, even though an estimation of groundwater resource was done based on different basic approaches in the region, basin wise groundwater numerical modeling has not been done, which is an effective approach to groundwater potential estimation and also reveals basic characteristics of the flow system. This can be of significant importance for the detailed understanding of available water resources and can contribute to the betterment of water resources planning and management. This study therefore attempts to produce a research output that can be useful for sustainable use of available groundwater resource.

Therefore, it can be drawn from the discussion above that, exploring sustainable and drought proof water resource is of significant importance. As an attempt to contribute to a suitable solution, this study focuses on evaluating the Genale-Dawa water resource potential and basic characterization of the ground water system. The study employs 3-D numerical ground water model to determine the monthly average groundwater table fluctuation and the replenishable groundwater potential of the basin which then is used to determine the amount of recharge/replenishable ground water potential. The result obtained is then combined with the result of groundwater potential result by base flow separation approach.

Various relevant raw data that can reveal an insight of the subsurface reservoir and software useful for modeling were collected. These are:

Software used for the model development, including;

• Mat lab v.13a: where numerical calculations are carried out and the TAGSAC code is run.

• Global Mapper v.16, Surfer v.10: used for surveying works, delineation, digitization, data manipulation and data preprocessing.

Hydrogeological data

• 1:2000,000 resolution geological map with 56 geological classes were collected.

• Location and static water level of springs, Bore holes and hand dug wells.

• 30 × 30 m resolution Digital elevation model of the region in which Genale-Dawa River basin is located.

Hydrological data

• Rain fall data records of 23 gauging stations near and on the basin.

• Stream flow data of some gauging station on the basin; this was used to develop an understanding of the overall hydro geological system and also, determine aquifer contribution to the rivers by performing base flow separation.

A particular type of FEM based three dimensional computer modeling code called TAGSAC (Three Dimensional Analysis of Groundwater Flow, Saitama University Code) is adopted for modeling the groundwater system. TAGSAC is a model developed for the porous medium. In the TAGSAC approximation procedure, the flow region is first discretized into a network of finite elements, and then trial approximating interpolation functions are generated for individual finite elements using a special type of weighted residual method called Galerkin’s method; in which the summation of residuals weighted by interpolation functions is equated to zero. This results in a system of linear interpolation functions. By incorporating boundary conditions and solving, coefficients of interpolation functions are obtained. This system of equations is used to represent the unknown dependent variable (hydraulic head) over the discretized region. A limiting feature of TAGSAC model is that it is bound to use a model thickness not less than half the finite elements dimension used; which otherwise will risk numerical instability. TAGSAC has proved to be applicable in a number of researches done all over the globe [

The geometric representation of the system shall first be established for which, Cartesian coordinate system is employed to generate a triangular in plane three dimensional mesh. The x-y plane coincides with plane view of the study area where as z direction point’s perpendicularly in the upward direction to the x-y plane; representing elevation.

An initial step taken for discretization was to delineate the Genale-Dawa catchment area which was done using Global Mapper version 16 and using digital elevation model of 30 × 30 m resolution. The result obtained was a little different than the official delineated map of Genale-Dawa river basin used by MOWE in that the delineation result obtained and to be used for this study has some additional area on the south-eastern part of the basin with a total of 17,860 km^{2}. This, in recent master plan study of the basin was recognized.

After the delineation x-y coordinates of the catchment boundary are generated and used as problem domain of the model. The discretization elements are made to be non-uniform in size to best fit the boundaries of the problem domain where there are Sharpe corners. A maximum of 5 km edge dimension for the equilateral triangular finite element is selected. This is done considering the available computational capacity and level of details of raw data available. The problem domain of 17,860 km^{2} area is then discretized in to 9810 nodes of known x-y coordinates with consistent and continuous nodal numbering assigned to them. 17,862 triangular elements are formed by connecting three neighboring nodes with a line. This geometric discretization of the region is first done on x-y plane and is carried out using automatic discretizing Mat lab computer code. The z coordinate of the nodal points of the mesh is tabulated by interpolation from the digital elevation model. After wards this triangular mesh so formed is given a model thickness of 2500 m to form a three dimensionally discretized region. Hence, each triangular two dimensional element was changed in to three dimensional finite element formed with six nodal points in space and becomes a prism that is triangular in plain. Boreholes and springs are represented by 3 nearest surface nodes whereas River systems are made to traverse along a series of surface nodes; this is done by moving the nearest surface node to the river at a point using a mat lab code. Relocation of the top layer nodes near a river causes vertical distortion of the prismatic finite elements that can be handled by TAGSAC.

Finally, individual elements and surface nodal points are given codes that designate the material property and rainfall recharge amount respectively to the individual elements and surface nodes.

Geological classes of the basin shown in

Several conceptual groundwater flow models have be distinguished on the basis

of the storage and flow capabilities of the porous medium and fracture. Among these, dual continuum, discrete fracture network, and single equivalent continuum types are the major once. Considering the vastness of the area under study and the extensive computational requirements associated with it, this study has adopted the single equivalent continuum approach to represent the geologic medium in the region. This allows finer representative elements to be used capturing the very high specially divers geological composition of Genale-Dawa river basin [

Hydraulic properties important for the three dimensional conceptual model include both horizontal and vertical hydraulic conductivities as well as specific storage coefficients. The distribution of these parameters must be specified for each geological unit. However since the model is based on the principles of equivalent porous medium, Hydraulic properties are assumed to be equivalent or effective values in the vertical extent for the 56 individual geological class. These geological classes have been discretized and Equivalent hydraulic properties are set as calibration parameters for respective geological classes.

Recharge is defined as the downward flow of water reaching the water table forming an addition to the ground water reservoir [

Major natural recharge to the aquifer system in the current study area is believed to occur at elevated regions due to percolation from the major precipitation areas along the north, north-eastern and north-western boundary highs of the basin. Whereas recharge from runoff and precipitation on the lower part of the basin also provides a source of groundwater inflow to the area of interest.

This study tries to estimate the replenishable groundwater resource (from hydrological perspective) using the TAGSAC model by seating precipitation to be some portion of the total rainfall in percent and making this percentage a calibration parameter that can be obtained through a series of trial and error procedure.

It is crucial to define boundary conditions prior to numerical groundwater model development. This is because, the solution of Laplace’s equation requires specification of boundary conditions which constrain the problem and make solutions unique [

1) Head is known for surfaces bounding the flow region (Dirichlet Conditions);

2) Flow is known across surfaces bounding the region (Newman condition);

3) A combination of Dirichlet and Newman conditions known as mixed condition.

The most common types of boundary conditions are; perennial rivers, springs, lakes and swampy areas known to have ground water reserve underneath, all of which can be taken as Dirichlet boundary conditions. On the other hand; known amount of inter-aquifer leakage, water wells and springs of known discharge can be taken as Newman’s conditions. The determination of which aspects of an actual ground-water system should be incorporated into a computer simulation usually depends, in part, upon the objectives of the study for which the model is being developed [

In the model calibration, simulated heads and discharges are typically compared to their observed counterparts. If a model is well calibrated, there will be some random deviations between simulated and observed data, but there will not be systematic deviations. If there are systematic deviations such as most simulated heads exceeding observed heads, the calibration is poor and adjustments should be made [

1) Qualitatively, by comparison of contour maps of measured and computed parameters, which provides only a qualitative measure of the similarity between the patterns; and

2) Quantitatively, by a scatter plot of measured and computed parameters, where the deviation of points from the straight line should be randomly distributed [

After the model calibration, monthly water table fluctuation is calculated. This helps determine the maximum water table, minimum water table and eventually the change in storage of the groundwater system within a year. This amount of water is known as the replenishable groundwater which represents the recharge capacity of the system. But, even though in a given month the aquifer is assumed to have a given amount of groundwater storage with an associated water table, it also discharges to the rivers at the same time. Hence, base flow separation is done using digital filter method to account for the water at the discharging end of the aquifer system and the cumulative groundwater reserve is calculated for individual months.

Finally based on calibration results hydraulic conductivities of different geologic classes are grouped to generate the different hydro-geologic classes of the region and prepare hydrogeologic map of the region.

All the discussion made in this chapter applies to the numerical model development of Genale-Dawa River Basin. The model protocol followed and work frame adapted to modeling of the basin can be represented with a flow diagram as shown in

Out of the collected Water point inventory data, some data was omitted for not qualifying to contain either the static water level or coordinate information. A secondary data screening was also done by comparing recorded static water level with expected result from the model. Accordingly, judgment was made to discard where large data inconsistency is observed. After screening 82 Bore holes, 49 hand dug wells and 191 spring data were left to be used as an input for the model. The distribution of water points used for model calibration is shown in

water points are located in the northern north-western and north-eastern parts of the basin which in general are topographically elevated areas. These parts of the basin are also the ones that receive majority of the precipitation and consequently expected to have majority of the recharge in the basin. On the other hand it can be seen that there is less concentration in the central and south-western parts of the basin. Therefore, even though there is uniformity absence in the distribution of water point for an ideal model calibration use, the fact that the distribution of water well data tends to be concentrated on parts of major recharging areas of the basin is fortunate and has a positive effect in capturing and conceptualizing the main features of the groundwater flow system for recharge potential estimation.

Determination of rainfall distribution over the basin is important prior to modeling in the groundwater potential assessment. It is used to approximate the amount of recharge from precipitation. Hence, Precipitation data of the study area was collected from Ethiopian National metrological Agency with a maximum of 15 years and a minimum of 10 years record. Data filling was done where there is missing. This was accomplished using a math lab program that uses the inverse distance method which was developed and coded by the authors of this study. The program is capable of dealing with a large amount of data; the Mat lab code of this program is attached in Appendix 4 for reference. After all fills were done; Point rainfall data is used to determine the spatial rainfall distribution over the entire basin. The Thiessen polygon generated for the Bore hole Hand dug well Spring Genale-Dawa River basin on the bases of 23 rain fall stations presented in

Monthly stream flow data of 12 gauging stations over the basin was collected. The length of data record ranges from 15 to 20 yrs. prior to using these data for the determination of base flow contribution to rivers, quality check was done using outlier testing. And data filling was done using single and multiple regression techniques alternatively for different stations. The choice of using either one was depending on the hydrological similarity between the gauging stations. After all the necessary data check and fills were done, digital filter method was employed to perform base flow separation of different stations. the result is shown in

Month | Station Name | Monthly Total (M^{3}) | |||||||||||
---|---|---|---|---|---|---|---|---|---|---|---|---|---|

Yadot | Welemel | Wyib | Togona | Mormora | Mesol | Mana | Healgo | Genale | Awata | Dimtu | Deyou | ||

Jan | 4.05 | 11.73 | 1.29 | 0.89 | 9.19 | 2.04 | 0.08 | 0.65 | 42.75 | 8.36 | 0.02 | 10.38 | 2742.50 |

Feb | 3.01 | 9.20 | 1.60 | 0.47 | 6.52 | 1.55 | 0.08 | 0.55 | 44.14 | 10.21 | 0.01 | 11.15 | 2654.48 |

Mar | 4.38 | 10.27 | 2.71 | 0.33 | 7.21 | 1.51 | 0.10 | 0.59 | 57.14 | 10.38 | 0.04 | 11.86 | 3195.32 |

Apr | 5.47 | 14.51 | 3.13 | 0.45 | 10.33 | 1.96 | 0.23 | 0.80 | 84.17 | 11.15 | 0.05 | 12.75 | 4350.28 |

May | 5.89 | 16.30 | 2.40 | 1.08 | 12.73 | 2.21 | 0.27 | 0.92 | 138.18 | 11.86 | 0.06 | 14.25 | 6184.58 |

Jun | 6.02 | 16.56 | 4.16 | 1.26 | 12.71 | 2.29 | 0.29 | 0.82 | 124.97 | 12.75 | 0.09 | 14.77 | 5900.45 |

Jul | 6.31 | 18.17 | 45.49 | 1.15 | 13.48 | 2.49 | 3.64 | 9.32 | 157.15 | 14.25 | 0.69 | 11.74 | 8516.10 |

Aug | 6.63 | 19.49 | 6.13 | 16.31 | 14.09 | 30.51 | 0.45 | 0.72 | 206.51 | 14.77 | 0.06 | 6.74 | 9672.67 |

Sep | 6.94 | 214.22 | 6.65 | 1.84 | 14.76 | 2.79 | 0.46 | 0.65 | 211.70 | 11.74 | 0.07 | 4.49 | 14289.19 |

Oct | 76.75 | 22.23 | 4.00 | 2.11 | 162.57 | 3.00 | 0.48 | 0.74 | 247.42 | 6.74 | 0.08 | 4.17 | 15909.17 |

Nov | 7.87 | 22.66 | 2.43 | 2.29 | 17.18 | 3.11 | 0.34 | 0.79 | 826.60 | 4.49 | 0.09 | 8.18 | 26881.03 |

Dec | 6.32 | 16.85 | 1.25 | 1.72 | 14.33 | 2.87 | 0.17 | 0.69 | 811.52 | 4.17 | 0.04 | 9.83 | 26092.85 |

Rivers as previously discussed are represented in the model with a set of nodal points that collectively make up the river system. Sections of rivers that cut through an aquifer to a considerable length have been identified in the region, they are considered as gaining rivers and in hydrological terms they are named Perennial Rivers; ones that do not dry throughout the season of the year. Some sections of the rivers that displayed such characteristics include Genale, Dawa, Gestro, Mena Weyeb and others small streams as well. These rivers, since they are gaining and are exposed to atmospheric pressure, can be taken as constant head boundaries (Dirichlet condition). Hence, the set of nodes that represent these rivers are set to have known hydraulic head equivalent to atmospheric head.

On the other hand, river sections that lose water to an aquifer are named losing or intermittent rivers. These types of rivers recharge the ground water with a loss rate that is variable spatially and temporally. They can be taken as specified flow boundary if the loss or gain rate of the stream is known spatially and temporally [

Moreover, the peripheral physical boundaries of the discretized region lie mostly on topographic highs locking the river basin, the regional groundwater divides are also assumed to align to these topographic conditions. Hence, it is assumed that the boundaries of the basin are no flow boundaries. In addition, the bottom surface of the region which in this study is taken to be 2500 km deep is assumed to have an impermeable bed making it a no flow boundary. At the same time, considering recharge due to precipitation is a major source to groundwater in the basin, this study also takes recharge rate into ground-water as a specified flow boundary condition along the top boundary of the groundwater model. The conceptual boundary conditions are presented in

After conceptualization of the flow system was complete and numerical model developed, TAGSAC model calibration was done by successively seating trial hydraulic conductivity values for individual geological classes until acceptable match was made between the historical hydraulic head record and simulated hydraulic head values. The resulting match was evaluated quantitatively using average indicators (AM, RMS, MAE) and qualitatively by comparison of groundwater contour maps generated with recorded and simulated hydraulic head data.

(A) Quantitative Check

1) The mean error (ME)

ME = 1 n ∑ i = 1 n ( h measured − h computed ) i = 3.91

2) The mean absolute error (MAE)

AME = 1 n ∑ i = 1 n | ( h measured − h computed ) i | = 7.46

3) The root mean squared error (RMS)

RMS = 1 n ∑ i = 1 n ( h measured − h computed ) i 2 = 10.65

(B) Qualitative check

From the qualitative comparison result presented by

model is calibrated and that the model represents the real system. Even though complete similarity is unachievable, a faire resemblance seems to exist. Considering the resolution of modeling and quality of data used, this result has been taken acceptable. The resulting horizontal and vertical hydraulic conductivity distribution for individual geologic classes are presented in

Groundwater table (piezometric head) of the region is calculated for each month in a year; using the calibrated model at nodal points. Afterwards conditions of possible maximum and possible minimum porosities of individual geologic mediums are taken. For each of these two conditions, monthly storage calculations in individual finite elements are done. The average of these tow conditions is used to determine groundwater table configuration in each month. This monthly groundwater table location showed seasonal fluctuation of the water table as shown in

The Ground water fluctuation trend seems to be comparable with rainfall series of the region for the most part, but near the 9th month it showed erratic behavior. This could be a cumulative result of a very complex geologic composition of the region and spatially non uniform rainfall pattern in the region.

In order to determine the total replenishable ground water reserve, monthly contribution of groundwater to rivers shall also be taken in to account. Accordingly base flow separation of stream flow data was done using single parameter digital filter approach (Appendix 1) and the result was added to the volume of replenishable ground water obtained from the model. This has resulted in 2.78 BM3 as total replenishable groundwater in Genale Dawa basin; the result is shown in

Geologic class code | Hydraulic Conductivity | |||
---|---|---|---|---|

Kx (m/s) | Ky (m/s) | Kz (m/s) | Keq | |

Ja | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Jg | 1.30E−05 | 1.30E−05 | 8.64E−05 | 1.20E−07 |

Jh1 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Jh2 | 1.73E−05 | 1.73E−05 | 2.16E−04 | 2.54E−07 |

Ka | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

kg1 | 8.64E−05 | 8.64E−06 | 2.16E−04 | 4.02E−07 |

kg2 | 7.78E−04 | 7.78E−04 | 8.56E−04 | 2.28E−05 |

Km | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Nb | 8.64E−04 | 8.64E−04 | 8.64E−05 | 8.03E−06 |

NMt | 8.64E−04 | 8.64E−05 | 8.64E−05 | 2.54E−06 |

NMv | 8.64E−04 | 8.64E−05 | 1.73E−04 | 3.59E−06 |

Nn | 8.64E−04 | 8.64E−05 | 1.73E−04 | 3.59E−06 |

Ntr2 | 8.64E−04 | 8.64E−05 | 8.64E−05 | 2.54E−06 |

Ntr3 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcdt | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcdt1 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcdt2 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcgb1 | 5.18E−04 | 5.18E−05 | 1.30E−04 | 1.87E−06 |

Pcgb2 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcgd | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Pcgn1 | 8.64E−08 | 8.64E−08 | 8.64E−08 | 2.54E−11 |

Pcgn2 | 8.64E−08 | 8.64E−08 | 4.32E−07 | 5.68E−11 |

Pcgn3 | 8.64E−08 | 8.64E−08 | 8.64E−08 | 2.54E−11 |

Pcgn4 | 8.64E−08 | 8.64E−08 | 8.64E−08 | 2.54E−11 |

Pcgn5 | 1.73E−07 | 2.33E−06 | 1.73E−08 | 8.35E−11 |

Pcgn6 | 8.64E−07 | 8.64E−09 | 8.64E−07 | 8.03E−11 |

Pcgn7 | 8.64E−07 | 8.64E−07 | 8.64E−08 | 2.54E−10 |

Pcgn8 | 8.64E−07 | 7.78E−05 | 4.32E−04 | 1.70E−07 |

Pcgn9 | 4.32E−06 | 7.78E−07 | 8.64E−07 | 1.70E−09 |

Pcgn10 | 8.64E−07 | 8.64E−07 | 2.16E−06 | 1.27E−09 |

Pcgn11 | 8.73E−07 | 1.30E−06 | 8.73E−07 | 9.94E−10 |

Pcgt1 | 4.75E−08 | 4.75E−08 | 8.64E−08 | 1.40E−11 |

Pcgt2 | 4.32E−07 | 4.32E−07 | 2.16E−07 | 2.01E−10 |

Pckb | 8.64E−07 | 8.64E−08 | 8.64E−08 | 8.03E−11 |

Pcs1 | 8.64E−08 | 8.64E−08 | 8.64E−08 | 2.54E−11 |

Pcs2 | 8.64E−08 | 8.64E−07 | 2.16E−07 | 1.27E−10 |
---|---|---|---|---|

Pcs3 | 8.64E−07 | 8.64E−07 | 8.64E−07 | 8.03E−10 |

Pcum1 | 8.64E−08 | 8.64E−08 | 8.64E−08 | 2.54E−11 |

Pcum2 | 8.64E−08 | 4.32E−07 | 8.64E−08 | 5.68E−11 |

Pcum3 | 8.64E−08 | 8.64E−07 | 8.64E−08 | 8.03E−11 |

Pcum4 | 8.64E−08 | 8.64E−08 | 8.64E−07 | 8.03E−11 |

PNb1 | 1.73E−04 | 1.73E−05 | 1.73E−05 | 2.27E−07 |

PNb2 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

PNi | 8.64E−05 | 1.30E−04 | 1.30E−04 | 1.20E−06 |

PNtr1 | 8.64E−08 | 8.64E−08 | 8.64E−07 | 8.03E−11 |

Q | 2.16E−03 | 2.16E−03 | 2.16E−03 | 1.00E−04 |

Q6 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Qa | 4.34E−03 | 4.34E−03 | 4.34E−03 | 2.86E−04 |

Qe | 1.30E−06 | 1.73E−06 | 1.73E−05 | 6.22E−09 |

Qv | 4.34E−04 | 4.34E−04 | 4.34E−04 | 9.03E−06 |

Qv1 | 1.73E−04 | 1.73E−03 | 2.16E−03 | 2.54E−05 |

Qv2 | 8.64E−05 | 8.64E−06 | 8.64E−05 | 2.54E−07 |

Qv3 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Qv4 | 8.64E−05 | 8.64E−05 | 2.16E−05 | 4.02E−07 |

Qv5 | 8.64E−05 | 8.64E−05 | 8.64E−05 | 8.03E−07 |

Tsy | 1.30E−04 | 8.64E−04 | 1.30E−04 | 3.81E−06 |

Month | Replenishable Ground Water (M^{3}) | Base Flow Contribution to Rivers (M^{3}) | Total Monthly Replenishable Ground Water (M^{3}) |
---|---|---|---|

Jan | 1.05E+08 | 2.74E+03 | 1.05E+08 |

Feb | 3.03E+08 | 2.65E+03 | 3.03E+08 |

Mar | 3.79E+08 | 3.20E+03 | 3.79E+08 |

Apr | 4.11E+08 | 4.35E+03 | 4.11E+08 |

May | 2.65E+08 | 6.18E+03 | 2.65E+08 |

Jun | 1.02E+08 | 5.90E+03 | 1.02E+08 |

Jul | 0.00E+00 | 8.52E+03 | 8.52E+03 |

Aug | 2.63E+08 | 9.67E+03 | 2.63E+08 |

Sep | 1.63E+08 | 1.43E+04 | 1.63E+08 |

Oct | 2.54E+08 | 1.59E+04 | 2.54E+08 |

Nov | 2.65E+08 | 2.69E+04 | 2.65E+08 |

Dec | 2.64E+08 | 2.61E+04 | 2.64E+08 |

Total Replenishable Ground Water | 2.78E+09 |

From the hydraulic conductivity values obtained from calibration it can be seen that many geological formations have similar hydraulic properties, for instance geologic mediums (Pcgn, Pcgn3, Pcgn4, Pcs1, Pcum1and Ja, Jh1, ka, km, Ntr3, Pcdt, Pcdt1, Pcdt2, Pcgb2, Pcgd, PNb2, Q6, Qv3, Qv5) have the same equivalent hydraulic conductivities where as others if not the same they have close similarity. Geologic characteristics of the Genale-Dawa River Basin can therefore be better understood if geologic mediums with similar hydraulic conductivity are grouped together. Accordingly, the following groups have been made and presented in

• High hydraulic conductivity geologic medium (>1 × 10^{−4} m/s);

• Moderately high hydraulic conductivity geologic medium (1 × 10^{−4} to 1 × 10^{−5} m/s);

• Moderately low hydraulic conductivity geologic medium (1 × 10^{−4} to 1 × 10^{−7} m/s);

• Low hydraulic conductivity geologic medium (1 × 10^{−7} to 1 × 10^{−12} m/s).

Additionally, by looking at the velocity field distribution it is possible to identify major recharging and discharging areas shown in

Groundwater modeling has versatile applications in groundwater resources

management that can be used for groundwater pollution management and more. This study used finite element based three dimensional groundwater modeling program called TAGSAC to estimate the groundwater recharge. The findings of this research showed that the basin has an average recharging potential of 2.78 BCM. However, further study on estimation of extraction factor shall be done. This factor accounts for the sociological, botanical and other concerned factors to determine the safest amount of groundwater that can be extracted from the basin. In addition, this study also attempted to characterize the groundwater flow system of the basin by preparing hydro-geological map and flow vector field, which can be useful in selection of well field in the future.

Based on the results obtained from the study the following recommendations are forwarded;

The identified sites of recharge area shall be protected from polluting chemicals to assure quality of the regions groundwater. Forestation of this area on the other hand can increase the available groundwater reserve by increasing the amount of infiltration and percolation; hence, it is recommended to plan and execute environmental protection projects in these regions.

Identified discharging areas can be used as well fields after carrying out the necessary detail investigation on the site. Therefore the regional authorities can consider ground water based water supply schemes for domestic and industrial purposes.

The authors declare no conflicts of interest regarding the publication of this paper.

Kassahun, N. and Mohamed, M. (2018) Groundwater Potential Assessment and Characterization of Genale-Dawa River Basin. Open Journal of Modern Hydrology, 8, 126-144. https://doi.org/10.4236/ojmh.2018.84010