# Comparative Hydrological and Geoelectrical Study on the Quaternary Aquifer in the Deltas of Wadi Badaa and Ghweiba, El Ain El Sukhna Area, Northwest Suez Gulf, Egypt

Authors: M. M. El Osta; A. El. El Sheikh; M. S. Barseem
Journal: International Journal of Geophysics
 (2010)

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## Abstract

El Ain El Sukhna area was selected in the last ten years to initiate many governmental and investmental programs. The different activities in that area depend mainly on the groundwater of the Quaternary aquifer, which forms the main water bearing strata. In the present work, twenty one geoelctrical soundings using the Schlumberger configuration are carried out at selected sites especially in missing parts from wells to delineate the groundwater setting in such sites. Eight of them are conducted in the close vicinity of water wells, where lithologs and pumping test data of these wells are available to relate hydrologic and geoelctric measurements. The pumping tests data are analyzed by using AQTESOLV program and the geolectrical sounding data were interpreted by partial curve matching technique to obtain the initial parameters. The results indicated that, the transmissivity is found to be closely related with transverse resistance and the hydraulic conductivity with average transverse resistivity, while the salinity is inversely related with resistivity. Finally, priority map for drilling water wells is constructed to make the results more illustrative and useful for decision maker. The promising area for drilling is located at the western portion of the study region.


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## Body

## 1. Introduction

The study area (390 km2) lies in the northwestern part of the Gulf of Suez between latitudes 29°38′ and 29°46′N and longitudes 32°08′ and 32°22′E (Figure 1). It is replenished by local rainfall, which is estimated to be of the order of 20 mm/year, as an average value of the two neighboring climatic stations, namely, Suez and St. Antony, over a period of about 25 years. Despite the fact that the annual rainfall is considered small, the area may occasionally receive heavy storms that may form considerable source for adequate replenishment, similar to those that took place in 1979 and 1981. In this area, many governmental activities such as the construction of El Sukhna port and many industrial zone as well as tourism projects are now under construction. So, the demand for water resources of appropriate quantity and quality is of vital importance. The development of groundwater resources and the regime of its activity largely depend on the hydraulic parameters of the water-bearing formation and water quality. The present work is carried out in the delta of both Wadi Ghweiba and Badaa in El Ain El Sukhna as an attempt to force investors to follow the complete scientific procedure for exploring the aquifer and defining the suitable sites to drill water wells. The evaluation of water-bearing formation comprises the quantity and quality by using geoelectrical techniques and confirms the results by hydrological studies to delineate: (1)
the sedimentary succession with its vertical and lateral facies changes,(2)
the water bearing formation, its extension, and hydraulic parameters,(3)
the groundwater quality.Figure 1
Map showing the location of the study area, wells, geoelectrical soundings (VES’es), and directions of cross sections.These are attained through the following activities (Figure1):(i)
inventory of 25 water wells in both Wadis,(ii)
performance of a set of 21 vertical electrical soundings (VES),(iii)
interpretation of obtainable 10 pumping test data.The different studies for geology, hydrogeology, and geophysics were carried out by a number of authors: Shata [3], Kostandy [4], Said [5, 6], UN [7], Cement Suez Company [8], Arabian Geophysics [9], Mostafa [10], Helal et al. [11], Abd Allatief et al. [12], Aboul Ela [13], El Houseiny [14], and Nasr [15]. Geomorphologically, the area under study represents an elongated depression with a general eastward slope towards the deltas of Wadi Ghawaiba and Badaa (coastal zone). It is bounded from the south and southwest by El Galala El Baharia plateau, from the west by Gebel El Khouder and Gebel El Ramliya and from the north by Gebel El Noqra and Gebel Ataqa (Figure 2). Geologically, the area located to the northwest of the Gulf of Suez is occupied by sedimentary rocks belonging to Quaternary, Pliocene, Miocene Oligocene, Eocene, Cretaceous, Jurassic, and Carboniferous (Figure 3). The Quaternary deposits (alluvial plain and wadi deposits) have a wide distribution in the study area. They are composed of gravels, sands, and shale.Figure 2
Map showing the main landforms in the study area (modified after Misak [1]).Figure 3
Geological map of the study area (Compiled after CONOCO [2]).


## 2. Hydrologic Setting

The Quaternary sand and gravel deposits form the main water-bearing strata in the Delta of both Wadi Badaa and Ghweiba having generally fresh to brackish water. It is represented by 25 drilled wells to pump water for companies, factories, and tourism villages distributed in the area. This aquifer is built up of sand and gravel with clay and limestone intercalations. The penetrated thickness of this aquifer reaches about 400 m at the mouth of Wadi Ghweiba and decreases towards north and northeast [16].The groundwater of the Quaternary aquifer occurs under free water table condition at depths varying between 9.4 m in the east and 39.9 m in the northwest. Its recharge depends mainly on the infiltration of surface runoff water and upward leakage from deep Pliocene and Miocene aquifers (see hydrogeological cross sections), while its discharge occurs either towards the Gulf of Suez or artificial pumping for different purposes (about 3000 m3/day). The determination of aquifer hydraulic parameters, transmissivity (T), and hydraulic conductivity (K) at constant discharge is done by analysis of pumping test data. These parameters are used to estimate the natural flow of water through the aquifer and its response to abstraction and to predict the aquifer yield and recharge. This can give preliminary information for further management of groundwater in the area. In the present study, the data of 10 long duration pumping tests are analyzed by using AQTESOLV program Version 4 [17] and by applying the following Cooper and Jacob formula [18]. The results are listed in Table 1(1)T=2.3Q/4πΔs,K=TH,
where T is the Transmissivity in m2/day, Q is the rate of discharge in m3/day, Δs is the slope in m, K is the regional hydraulic conductivity in m/day, and H is the saturated thickness in meter.Table 1
Results of hydraulic parameters estimation of the Quaternary aquifer in the deltas of Wadi Badaa and Ghweiba.
Well no.Saturated thickness (m)TransmissivityT (m2/day)Hydraulic ConductivityK (m/day)599.1507.75.123696380.33.9611297.5655.596.7241499990.2510.001694378.074.0221899.9755.37.5622101.1857.688.482390.6692.997.642479318.5284.0322578.4698.128.90The graphical representation of pumping test data is explained by that of well no. 18 as shown in Figure4. The obtained parameters from all wells revealed values ranging from 318.528 m2/day (well no. 24) to 990.25 m2/day (well no. 14) for transmissivity and from 3.961 m/day (well no. 6) to 10 m/day (well no. 14) for hydraulic conductivity. The narrow range of both T and K is mainly attributed to the slight lateral facies changes as well as the similarity of the saturated thickness of the aquifer.Figure 4
Analysis of data of pumping test for well no. 18 (Wadi Badaa).


## 3. Groundwater Quality Assessment

The salinity measurements of groundwater in the Quaternary aquifer indicate that it belongs to the slightly fresh to brackish water class according to Chebotarev classification [19–21], where the TDS ranges between 560 mg/l (well no. 21) and 4670 mg/l (well no. 23). Generally, the higher values of TDS are recorded towards the Gulf of Suez (Figure 5), which indicates more developed stage of chemical composition along the flow path from the upstreams to downstreams of both Wadis. This takes place on account of leaching, dissolution and ion exchange processes. The isotopic investigation carried out by Desouki et al. [16] indicates that the recharge of this aquifer depends mainly on the infiltration of surface runoff and upward leakage from deep aquifers.Figure 5
Iso-salinity distribution contour map of the deltas of Wadi Badaa and Ghweiba (Augusts, 2009).


## 4. Geoelectrical Soundings

### 4.1. Sounding Curves

Twenty one vertical electrical sounding were carried out in the investigated area especially in missing parts from wells as in (Figure1) to delineate the groundwater setting in these localities. Some of the VES stations (nos. 1, 6, 7, 14, 15, 19, 20, and 21) are conducted in the close vicinity of water wells (nos. 12, 16, 14, 18, 22, 25, 23, and 24), respectively, where lithologs and pumping test data of these wells are available. The Schlumberger electrode configuration was used in VES measurements with maximum electrode separation with a current electrodes separation (AB) starting by 1 meter and ending with 1400 to 2000 meters using terremater SAS 300 and SAS 100 resistivitymeter. The instrument directly measures the resistance with high accuracy. The calculated apparent resistivity is plotted against the corresponding half the electrode separation (AB/2) to construct the VES curves (Figure 6). A land topographic surveying was also carried out in order to determine the accurate locations and ground elevations of the sounding station.Examples of the resistivity sounding curves.
(a)(b)


### 4.2. Interpretation of the VES Measurements

The purpose of the VES measurements was to determine the geoelectrical parameters of series subsurface layer. The qualitative and quantitative interpretations of the geoelectrical sounding data are discussed in terms of geoelectrical parameters of resulting layer (resistivities and thicknesses) as follows.


#### 4.2.1. Qualitative Interpretation

The qualitative interpretation includes comparison of the relative changes in the apparent resistivity and thickness of the detected layer on the sounding curves. It gives information about the number of layers, their continuity through the area and reflects the degree of homogeneity or heterogeneity of an individual layer. Figure6 shows an example of the field representations of the measured VES along the area of study. These soundings are characterized by high resistivity values in the first cycle (AB=10) reflecting a dry zone (gravel and sand), but the differences are clear in the last cycle (AB>10) reflecting the effect of groundwater on the geophysical parameters (resistivities) as well as the variation in the depths of the layers and their nature. The curves in the delta of Wadi Badda are terminated by Q-type (ended by low resistivity values) which reflects the increase of water salinity. On the other hand, the curves of the delta Wadi Ghweiba are ended by H-type (high resistivity values) reflecting the presence of limestone deposits.


#### 4.2.2. Quantitative Interpretation

The field data of VES has been interpreted quantitatively using the computer program “RESIST” of Van Der Velpen [22] to delineate the subsurface succession of the geoelectrical layers in the area. The initial model has constructed in the view of the lithologic succession of the existed wells. The parameter of the best fit curves, for example, depth, thickness, and resistivity of each layer, are then taken to represent the final interpretation model for the corresponding sounding curves. In order to reach optimum correlation between the geoelectrical layers and the predominant geologic units, some successive geoelectrical layers (mostly the upper most ones) have been grouped together in one layer. The resistivity of such a layer is expressed in terms of the average transverse resistivity (pt). The true resistivities are related to the geologic information of the existed drilled wells. Figure 7 shows the interpretation of the model resistivity sounding VES no. 20 beside the drilled well no. 23.Figure 7
Interpretation modeled of VES no. 20.


### 4.3. Results and Discussion

The common features characterizing the lithologies and hydrological properties in the investigated area are described in view of constructed hydrogeological cross sections and maps. The comparison between the interpreted data of the VES and the lithology as well as information of some drilled wells revealed that the geoelectrical succession of the area under study consists of three geoelectrical layers, which have been referred to as A, B and C. The geoelectrical parameters, resistivities and thicknesses are tabulated in Table2.Table 2
The ranges of the resistivities and the corresponding thicknesses of the geoelectrical layers.
Geoelectrical layerResistivity range (Ohm·m)Thickness range (m)Lithological descriptionMinimumMaximumMinimumMaximumA140306050.93.1Surface layerB127506.5738.6Dry Quaternary deposit (sand and gravels)B221.0245.878.4101.7Saturated Quaternary zone consist from clayey sandC12.89.71725.5clayey sand & gravelsSaturated Pliocene-MioceneC247110.3——LimestoneThree hydrogeological cross sections have been constructed based on the interpreted data of the VESs and lithologic data of wells (Figures8, 9, and 10). These sections illustrate the sedimentary succession, lateral, and vertical resistivity that reflects the lithology changes of the different layers as follows. (i)
The first layer (A) consists of dry sediments such as sand, gravel, and clay belonging to the Quaternary period. This layer shows its maximum resistivity value at VES no. (18) (30605 Ohm·m.) whereas its minimum resistivity is recorded at VES no. (6) (140 Ohm·m). This layer exhibits a thickness which does not exceed 3 m.(ii)
The second layer (B) consists of calcareous and clayey sand, gravel, and shale related to Quaternary, according to the lithology and well information at VES no. (20). It can be divided into an upper part (B1) and a lower are (B2). The upper (B1) is dry and its resistivity ranges between 27 Ohm·m at VES no. (5) and 506.5 Ohm·m at VES no. (7). The thickness of this part ranges between 7 m at VES no. (5) and 38.6 m at VES no. (8). The lower part (B2) is saturated with water and it consists of from three geoelectrical layers according to the lithologic information of wells. These three layers can be gathered in one zone and expressed in terms of an average transverse resistivity (pt). It shows resistivity ranges from 21.05 Ohm·m at VES no. (17) to 45.8 Ohm·m at VES no. (18). This part reaches its minimum thickness (78.4 m) at VES no. (19) and well no. (25) while its maximum thickness (101.7 m.) at VES no. (10).(iii)
The last detected layer (C) is saturated and divided into two parts (C1) and (C2) belonging to Pliocene-Miocene ages. The upper part (C1) is composed from clayey sand and gravel. Its resistivity value ranges from 2.8 Ohm·m at VES no. (1) to 9.7 Ohm·m at VES no. (15). The thickness of this part varies from 17 m at VES no. (20) to 25.5 m at VES no. (15). The lower part (C2) is detected at some sound. This layer corresponds to saturated limestone and shows resistivity varies from 47 Ohm·m at VES no. (5) to 110 Ohm·m at VES no. (17).Figure 8
West-East hydrogeological cross sectionA-A′.Figure 9
West-East hydrogeological cross sectionB-B′.Figure 10
North-South hydrogeological cross sectionC-C′.According to the geoelectrical results and lithologic information of drilled wells, the Quaternary aquifer represents the major promising aquifer in the study area. It consists of calcareous and clayey sand, gravel, and shale acting as first water bearing zone. On the other hand, the Pliocene-Miocene aquifer is divided into two parts (C1 & C2). The upper one corresponds to clayey sand and gravel, and the lower one is represented by limestone. The iso-resistivity contour map of the Quaternary aquifer (Figure11) shows a general decrease in resistivity value eastward direction (Gulf of Suez), which indicates poor water quality (high salinity and or high clay content). Also, the spatial distribution of the thickness for this aquifer is illustrated in (Figure 12). This map shows gradual decrease in thickness from northwest to east and southeastern direction.Figure 11
Iso-resistivity contour map of the Quaternary aquifer (B2).Figure 12
Isopach contour map of the Quaternary aquifer (B2).


### 4.4. Predicted Hydraulic Parameters of the Quaternary Aquifer

The estimation of aquifer characteristics can be offered by surface geoelectrical measurements. This approach is based on the fact that the electric current follows the path of least resistance, as water does within and around the rock pores. The mode of conduction of electrcity is ionic and the resistivity of the medium controlled by porosity and water conductivity based on the rock matrix. Thus, at the pore level, the electrical path, is similar to the hydraulic path and the resistivity should reflect the hydraulic conductivity. The similarity in the behavior of the electrical path through a medium with the hydraulic path is definitions of the electric and hydraulic parameters. The total transverse unit resistance (Tρ) is given by (2)Tρ=∑hi*pi,
where hi and pi are the thickness and resistivity of ith layer in the section, respectively.Also, the transmissivity (T) is represented by the relation (3)T=∑hi*Ki,
where hi and Ki are the thickness and resistivity of ith layer in the section, respectively.The average transverse resistivity (Pt) is given by (4)Pt=∑pi*hi∑hi.
And the hydraulic conductivity (K) is given by(5)K=∑Ki*hi∑hi.These model parameters are used to obtain the transmissivities from the corresponding transverse resistance and the hydraulic conductivities from the corresponding average transverse resistivities. According to the interpretation of each sounding curve, the transverse resistance and the average transverse resistivity have been calculated and listed in Table3. Several works, to establish empirical relationships between various aquifer hydraulic parameters obtained both from pumping test analysis and geoelectrical measurement have been carried out by Kelly [23] who establishes an empirical relation between aquifer electrical resistivity (Pt) and hydraulic conductivity (K). Also, Mbonu et al. [24] calculated aquifer hydraulic conductivity and transmissivity from the model obtained from the interpretation of geoelectrical sounding in part of the Umuahia area of Nigeria. In the present work, the following empirical relationships between geoelectrical and hydraulic parameters are constructed.Table 3
Geoelectrical parameters and predicted transmissivity, hydraulic conductivity, and salinity of the Quaternary aquifer from the Vertical Electrical Soundings (VESs).
VES no.Ground elevat. (±m)Depth to water (m)Water table (m)Saturated thickness (m)Tp (Ohm·m2)Pt (Ohm·m)PredictedT (m2/day)PredictedK (m/day)Predicted TDS (mg/l)*12724.82.297.5350135.91772.9597.8612107.6422220292.53365.436.38739.0327.9822045.3331918198.52451.224.89510.2955.0233568.4341715.51.5101.52344.5623.10483.6144.5623805.715229.412.696.82400.824.80497.6855.003580.36*61013.3−3.394201921.48402.1574.1444020.45*74238.53.597437745.12992.13810.233886.7784339.93.195.23133.832.92681.0857.0912503.9992320.12.997.92282.1223.31467.9914.6163777.87102017.52.5101.72649.1726.05559.8285.3223414.661121174101.42948.629.08634.7476.1023013.01122319.93.199.53190.1232.06695.1766.872546.40132120.71.3100.13312.7933.09725.8687.1352481.45*142119299.93284.6132.88718.8187.0812509.29*154223.318.7101.13729.8536.89830.2198.1141977.73163722.814.294.62831.6229.93605.4786.3212900.34173518.616.488185021.02359.8734.0264081.431834221295.44364.645.75989.03610.396803.26*193022878.4303638.72656.6158.5851735.15*203416.717.390.63013.6633.26651.0257.1792458.92*212915.213.879170121.53322.594.1574013.8Where:is* well beside VES, Tp is transverse resistance, Pt is average transverse resistivity, T is transmissivity, K is hydraulic conductivity, and TDS is total dissolved solids.


#### 4.4.1. Relation between Transmissivity and Transverse Resistance

The relation between transmissivity (T) obtained from pumping test analysis for 8 wells and computed transverse resistance (Tρ) of the aquifer from vertical electrical soundings beside these wells is shown in Figure 13. This plot confirms the dependance of T with Tρ as T=0.2502039523*Tρ-103.0039872 with coefficient of determination of 0.943868. Accordingly, the transmissivity is found to be closely related with transverse resistance which is in agreement with the earlier work done by Frohlich and Kelly [25].Figure 13
Relation between transmissivity and transverse resistance.


#### 4.4.2. Relation between Hydraulic Conductivity and Average Transverse Resistivity

The hydraulic conductivity (K) values have been plotted versus the average transverse resistivity (Pt). These plots and their best fit are shown in Figure 14. The specific empirical equation for this relation has been established as K=0.25755678929*Pt-1.38762128 with coefficient of determination of 0.937837.Figure 14
Relation between hydraulic conductivity and average transverse resistivity.


#### 4.4.3. Relation between Salinity and Average Transverse Resistivity

The decrease of resistivity values is considered as an indication of increase of either clay content and/or water salinity (both two factors led to poor water quality). In the present work, the relation between the recorded resistivity values from electrical soundings and the corresponding salinity (TDS) values beside wells are plotted in Figure15. This plot shows the confidence of TDS with Pt as TDS=-132.558449*Pt+6867.81438 with coefficient of determination of 0.840022. The slope of line is negative which indicates the decrease in salinity with an increase in the resistivity. It should be mentioned here that the aquifer resistivity of water is not only a function of salinity but also of clay content besides the packing and grain size. Therefore, the above established empirical equations have been utilized in predicting the hydraulic parameters and salinity in all vertical electrical sounding sites in the study area (Table 3), which are used as preliminary information for drilling water wells and further management of groundwater supply of the area.Figure 15
Relation between TDS and average transverse resistivity.


## 4.1. Sounding Curves

Twenty one vertical electrical sounding were carried out in the investigated area especially in missing parts from wells as in (Figure1) to delineate the groundwater setting in these localities. Some of the VES stations (nos. 1, 6, 7, 14, 15, 19, 20, and 21) are conducted in the close vicinity of water wells (nos. 12, 16, 14, 18, 22, 25, 23, and 24), respectively, where lithologs and pumping test data of these wells are available. The Schlumberger electrode configuration was used in VES measurements with maximum electrode separation with a current electrodes separation (AB) starting by 1 meter and ending with 1400 to 2000 meters using terremater SAS 300 and SAS 100 resistivitymeter. The instrument directly measures the resistance with high accuracy. The calculated apparent resistivity is plotted against the corresponding half the electrode separation (AB/2) to construct the VES curves (Figure 6). A land topographic surveying was also carried out in order to determine the accurate locations and ground elevations of the sounding station.Examples of the resistivity sounding curves.
(a)(b)


## 4.2. Interpretation of the VES Measurements

The purpose of the VES measurements was to determine the geoelectrical parameters of series subsurface layer. The qualitative and quantitative interpretations of the geoelectrical sounding data are discussed in terms of geoelectrical parameters of resulting layer (resistivities and thicknesses) as follows.


### 4.2.1. Qualitative Interpretation

The qualitative interpretation includes comparison of the relative changes in the apparent resistivity and thickness of the detected layer on the sounding curves. It gives information about the number of layers, their continuity through the area and reflects the degree of homogeneity or heterogeneity of an individual layer. Figure6 shows an example of the field representations of the measured VES along the area of study. These soundings are characterized by high resistivity values in the first cycle (AB=10) reflecting a dry zone (gravel and sand), but the differences are clear in the last cycle (AB>10) reflecting the effect of groundwater on the geophysical parameters (resistivities) as well as the variation in the depths of the layers and their nature. The curves in the delta of Wadi Badda are terminated by Q-type (ended by low resistivity values) which reflects the increase of water salinity. On the other hand, the curves of the delta Wadi Ghweiba are ended by H-type (high resistivity values) reflecting the presence of limestone deposits.


### 4.2.2. Quantitative Interpretation

The field data of VES has been interpreted quantitatively using the computer program “RESIST” of Van Der Velpen [22] to delineate the subsurface succession of the geoelectrical layers in the area. The initial model has constructed in the view of the lithologic succession of the existed wells. The parameter of the best fit curves, for example, depth, thickness, and resistivity of each layer, are then taken to represent the final interpretation model for the corresponding sounding curves. In order to reach optimum correlation between the geoelectrical layers and the predominant geologic units, some successive geoelectrical layers (mostly the upper most ones) have been grouped together in one layer. The resistivity of such a layer is expressed in terms of the average transverse resistivity (pt). The true resistivities are related to the geologic information of the existed drilled wells. Figure 7 shows the interpretation of the model resistivity sounding VES no. 20 beside the drilled well no. 23.Figure 7
Interpretation modeled of VES no. 20.


## 4.2.1. Qualitative Interpretation

The qualitative interpretation includes comparison of the relative changes in the apparent resistivity and thickness of the detected layer on the sounding curves. It gives information about the number of layers, their continuity through the area and reflects the degree of homogeneity or heterogeneity of an individual layer. Figure6 shows an example of the field representations of the measured VES along the area of study. These soundings are characterized by high resistivity values in the first cycle (AB=10) reflecting a dry zone (gravel and sand), but the differences are clear in the last cycle (AB>10) reflecting the effect of groundwater on the geophysical parameters (resistivities) as well as the variation in the depths of the layers and their nature. The curves in the delta of Wadi Badda are terminated by Q-type (ended by low resistivity values) which reflects the increase of water salinity. On the other hand, the curves of the delta Wadi Ghweiba are ended by H-type (high resistivity values) reflecting the presence of limestone deposits.


## 4.2.2. Quantitative Interpretation

The field data of VES has been interpreted quantitatively using the computer program “RESIST” of Van Der Velpen [22] to delineate the subsurface succession of the geoelectrical layers in the area. The initial model has constructed in the view of the lithologic succession of the existed wells. The parameter of the best fit curves, for example, depth, thickness, and resistivity of each layer, are then taken to represent the final interpretation model for the corresponding sounding curves. In order to reach optimum correlation between the geoelectrical layers and the predominant geologic units, some successive geoelectrical layers (mostly the upper most ones) have been grouped together in one layer. The resistivity of such a layer is expressed in terms of the average transverse resistivity (pt). The true resistivities are related to the geologic information of the existed drilled wells. Figure 7 shows the interpretation of the model resistivity sounding VES no. 20 beside the drilled well no. 23.Figure 7
Interpretation modeled of VES no. 20.


## 4.3. Results and Discussion

The common features characterizing the lithologies and hydrological properties in the investigated area are described in view of constructed hydrogeological cross sections and maps. The comparison between the interpreted data of the VES and the lithology as well as information of some drilled wells revealed that the geoelectrical succession of the area under study consists of three geoelectrical layers, which have been referred to as A, B and C. The geoelectrical parameters, resistivities and thicknesses are tabulated in Table2.Table 2
The ranges of the resistivities and the corresponding thicknesses of the geoelectrical layers.
Geoelectrical layerResistivity range (Ohm·m)Thickness range (m)Lithological descriptionMinimumMaximumMinimumMaximumA140306050.93.1Surface layerB127506.5738.6Dry Quaternary deposit (sand and gravels)B221.0245.878.4101.7Saturated Quaternary zone consist from clayey sandC12.89.71725.5clayey sand & gravelsSaturated Pliocene-MioceneC247110.3——LimestoneThree hydrogeological cross sections have been constructed based on the interpreted data of the VESs and lithologic data of wells (Figures8, 9, and 10). These sections illustrate the sedimentary succession, lateral, and vertical resistivity that reflects the lithology changes of the different layers as follows. (i)
The first layer (A) consists of dry sediments such as sand, gravel, and clay belonging to the Quaternary period. This layer shows its maximum resistivity value at VES no. (18) (30605 Ohm·m.) whereas its minimum resistivity is recorded at VES no. (6) (140 Ohm·m). This layer exhibits a thickness which does not exceed 3 m.(ii)
The second layer (B) consists of calcareous and clayey sand, gravel, and shale related to Quaternary, according to the lithology and well information at VES no. (20). It can be divided into an upper part (B1) and a lower are (B2). The upper (B1) is dry and its resistivity ranges between 27 Ohm·m at VES no. (5) and 506.5 Ohm·m at VES no. (7). The thickness of this part ranges between 7 m at VES no. (5) and 38.6 m at VES no. (8). The lower part (B2) is saturated with water and it consists of from three geoelectrical layers according to the lithologic information of wells. These three layers can be gathered in one zone and expressed in terms of an average transverse resistivity (pt). It shows resistivity ranges from 21.05 Ohm·m at VES no. (17) to 45.8 Ohm·m at VES no. (18). This part reaches its minimum thickness (78.4 m) at VES no. (19) and well no. (25) while its maximum thickness (101.7 m.) at VES no. (10).(iii)
The last detected layer (C) is saturated and divided into two parts (C1) and (C2) belonging to Pliocene-Miocene ages. The upper part (C1) is composed from clayey sand and gravel. Its resistivity value ranges from 2.8 Ohm·m at VES no. (1) to 9.7 Ohm·m at VES no. (15). The thickness of this part varies from 17 m at VES no. (20) to 25.5 m at VES no. (15). The lower part (C2) is detected at some sound. This layer corresponds to saturated limestone and shows resistivity varies from 47 Ohm·m at VES no. (5) to 110 Ohm·m at VES no. (17).Figure 8
West-East hydrogeological cross sectionA-A′.Figure 9
West-East hydrogeological cross sectionB-B′.Figure 10
North-South hydrogeological cross sectionC-C′.According to the geoelectrical results and lithologic information of drilled wells, the Quaternary aquifer represents the major promising aquifer in the study area. It consists of calcareous and clayey sand, gravel, and shale acting as first water bearing zone. On the other hand, the Pliocene-Miocene aquifer is divided into two parts (C1 & C2). The upper one corresponds to clayey sand and gravel, and the lower one is represented by limestone. The iso-resistivity contour map of the Quaternary aquifer (Figure11) shows a general decrease in resistivity value eastward direction (Gulf of Suez), which indicates poor water quality (high salinity and or high clay content). Also, the spatial distribution of the thickness for this aquifer is illustrated in (Figure 12). This map shows gradual decrease in thickness from northwest to east and southeastern direction.Figure 11
Iso-resistivity contour map of the Quaternary aquifer (B2).Figure 12
Isopach contour map of the Quaternary aquifer (B2).


## 4.4. Predicted Hydraulic Parameters of the Quaternary Aquifer

The estimation of aquifer characteristics can be offered by surface geoelectrical measurements. This approach is based on the fact that the electric current follows the path of least resistance, as water does within and around the rock pores. The mode of conduction of electrcity is ionic and the resistivity of the medium controlled by porosity and water conductivity based on the rock matrix. Thus, at the pore level, the electrical path, is similar to the hydraulic path and the resistivity should reflect the hydraulic conductivity. The similarity in the behavior of the electrical path through a medium with the hydraulic path is definitions of the electric and hydraulic parameters. The total transverse unit resistance (Tρ) is given by (2)Tρ=∑hi*pi,
where hi and pi are the thickness and resistivity of ith layer in the section, respectively.Also, the transmissivity (T) is represented by the relation (3)T=∑hi*Ki,
where hi and Ki are the thickness and resistivity of ith layer in the section, respectively.The average transverse resistivity (Pt) is given by (4)Pt=∑pi*hi∑hi.
And the hydraulic conductivity (K) is given by(5)K=∑Ki*hi∑hi.These model parameters are used to obtain the transmissivities from the corresponding transverse resistance and the hydraulic conductivities from the corresponding average transverse resistivities. According to the interpretation of each sounding curve, the transverse resistance and the average transverse resistivity have been calculated and listed in Table3. Several works, to establish empirical relationships between various aquifer hydraulic parameters obtained both from pumping test analysis and geoelectrical measurement have been carried out by Kelly [23] who establishes an empirical relation between aquifer electrical resistivity (Pt) and hydraulic conductivity (K). Also, Mbonu et al. [24] calculated aquifer hydraulic conductivity and transmissivity from the model obtained from the interpretation of geoelectrical sounding in part of the Umuahia area of Nigeria. In the present work, the following empirical relationships between geoelectrical and hydraulic parameters are constructed.Table 3
Geoelectrical parameters and predicted transmissivity, hydraulic conductivity, and salinity of the Quaternary aquifer from the Vertical Electrical Soundings (VESs).
VES no.Ground elevat. (±m)Depth to water (m)Water table (m)Saturated thickness (m)Tp (Ohm·m2)Pt (Ohm·m)PredictedT (m2/day)PredictedK (m/day)Predicted TDS (mg/l)*12724.82.297.5350135.91772.9597.8612107.6422220292.53365.436.38739.0327.9822045.3331918198.52451.224.89510.2955.0233568.4341715.51.5101.52344.5623.10483.6144.5623805.715229.412.696.82400.824.80497.6855.003580.36*61013.3−3.394201921.48402.1574.1444020.45*74238.53.597437745.12992.13810.233886.7784339.93.195.23133.832.92681.0857.0912503.9992320.12.997.92282.1223.31467.9914.6163777.87102017.52.5101.72649.1726.05559.8285.3223414.661121174101.42948.629.08634.7476.1023013.01122319.93.199.53190.1232.06695.1766.872546.40132120.71.3100.13312.7933.09725.8687.1352481.45*142119299.93284.6132.88718.8187.0812509.29*154223.318.7101.13729.8536.89830.2198.1141977.73163722.814.294.62831.6229.93605.4786.3212900.34173518.616.488185021.02359.8734.0264081.431834221295.44364.645.75989.03610.396803.26*193022878.4303638.72656.6158.5851735.15*203416.717.390.63013.6633.26651.0257.1792458.92*212915.213.879170121.53322.594.1574013.8Where:is* well beside VES, Tp is transverse resistance, Pt is average transverse resistivity, T is transmissivity, K is hydraulic conductivity, and TDS is total dissolved solids.


### 4.4.1. Relation between Transmissivity and Transverse Resistance

The relation between transmissivity (T) obtained from pumping test analysis for 8 wells and computed transverse resistance (Tρ) of the aquifer from vertical electrical soundings beside these wells is shown in Figure 13. This plot confirms the dependance of T with Tρ as T=0.2502039523*Tρ-103.0039872 with coefficient of determination of 0.943868. Accordingly, the transmissivity is found to be closely related with transverse resistance which is in agreement with the earlier work done by Frohlich and Kelly [25].Figure 13
Relation between transmissivity and transverse resistance.


### 4.4.2. Relation between Hydraulic Conductivity and Average Transverse Resistivity

The hydraulic conductivity (K) values have been plotted versus the average transverse resistivity (Pt). These plots and their best fit are shown in Figure 14. The specific empirical equation for this relation has been established as K=0.25755678929*Pt-1.38762128 with coefficient of determination of 0.937837.Figure 14
Relation between hydraulic conductivity and average transverse resistivity.


### 4.4.3. Relation between Salinity and Average Transverse Resistivity

The decrease of resistivity values is considered as an indication of increase of either clay content and/or water salinity (both two factors led to poor water quality). In the present work, the relation between the recorded resistivity values from electrical soundings and the corresponding salinity (TDS) values beside wells are plotted in Figure15. This plot shows the confidence of TDS with Pt as TDS=-132.558449*Pt+6867.81438 with coefficient of determination of 0.840022. The slope of line is negative which indicates the decrease in salinity with an increase in the resistivity. It should be mentioned here that the aquifer resistivity of water is not only a function of salinity but also of clay content besides the packing and grain size. Therefore, the above established empirical equations have been utilized in predicting the hydraulic parameters and salinity in all vertical electrical sounding sites in the study area (Table 3), which are used as preliminary information for drilling water wells and further management of groundwater supply of the area.Figure 15
Relation between TDS and average transverse resistivity.


## 4.4.1. Relation between Transmissivity and Transverse Resistance

The relation between transmissivity (T) obtained from pumping test analysis for 8 wells and computed transverse resistance (Tρ) of the aquifer from vertical electrical soundings beside these wells is shown in Figure 13. This plot confirms the dependance of T with Tρ as T=0.2502039523*Tρ-103.0039872 with coefficient of determination of 0.943868. Accordingly, the transmissivity is found to be closely related with transverse resistance which is in agreement with the earlier work done by Frohlich and Kelly [25].Figure 13
Relation between transmissivity and transverse resistance.


## 4.4.2. Relation between Hydraulic Conductivity and Average Transverse Resistivity

The hydraulic conductivity (K) values have been plotted versus the average transverse resistivity (Pt). These plots and their best fit are shown in Figure 14. The specific empirical equation for this relation has been established as K=0.25755678929*Pt-1.38762128 with coefficient of determination of 0.937837.Figure 14
Relation between hydraulic conductivity and average transverse resistivity.


## 4.4.3. Relation between Salinity and Average Transverse Resistivity

The decrease of resistivity values is considered as an indication of increase of either clay content and/or water salinity (both two factors led to poor water quality). In the present work, the relation between the recorded resistivity values from electrical soundings and the corresponding salinity (TDS) values beside wells are plotted in Figure15. This plot shows the confidence of TDS with Pt as TDS=-132.558449*Pt+6867.81438 with coefficient of determination of 0.840022. The slope of line is negative which indicates the decrease in salinity with an increase in the resistivity. It should be mentioned here that the aquifer resistivity of water is not only a function of salinity but also of clay content besides the packing and grain size. Therefore, the above established empirical equations have been utilized in predicting the hydraulic parameters and salinity in all vertical electrical sounding sites in the study area (Table 3), which are used as preliminary information for drilling water wells and further management of groundwater supply of the area.Figure 15
Relation between TDS and average transverse resistivity.


## 5. Priority of Water Well Drilling

In order to make the aforementioned results (Table3) more illustrative and useful for decision makers, a priority map has been presented. The generation of this map depends on the mutual effect of TDS, thickness, transmissivity, and hydraulic conductivity through the saturated layer in the study area besides the depth of water. The collective effects of the saturated layer have been presented to show priority zones in the study region. The saturated layer is characterized by approximately uniform thickness so their weight factor is 10%. The TDS, depth to water, transmissivity, and hydraulic conductivity play a significant role in groundwater utilization. Consequently, their weight factors are 30%, 20%, 20%, and 20%, respectively. These factors are essential for the construction of the priority map. The above parameters have been classified into four categories (Table 4).Table 4
The thickness, TDS, depth to water, transmissivity, and hydraulic conductivity category ranges for the saturated layer (B2).
CategoryThickness ranges (m)TDS ranges (mg/l)Depth to water ranges (m)TransmissivityT (m2/day)Hydraulic conductivityK (m/day)1≥95≤900≤20>850>92>90 ≤95>900 ≤500>20 ≤30>500 ≤850>6 ≤93>80 ≤90>1500 ≤3000>30 ≤35>400 ≤500>5 ≤64<80>3000>35<400<5According to the priority map (Figure16), it could be concluded that the promising area for drilling water wells is located at the western portion. The priority of groundwater quality and potentiality decrease towards the eastern portion of the concerned area.Figure 16
Priority map for drilling water wells in the study area.


## 6. Conclusions

In the deltas of Wadi Badaa and Ghweiba, the Quaternary aquifer forms the major promising aquifer having generally fresh to brackish water. It is built up of sand and gravel with clay and limestone intercalations. This succession overlies directly the Pliocene-Miocene deposits. The groundwater exists under free water table condition at a depth that varies from 39.9 m in the northwest to 9.4 m in the east below ground surface. The values of the transmissivity of the Quaternary aquifer range from 318.528 m2/day to 990.25 m2/day, and the hydraulic conductivity varies from 3.961 m/day to 10 m/day. The groundwater belongs to the slightly fresh to brackish water class, where the TDS ranges between 560 mg/l and 4670 mg/l. The results of geoelectrical soundings conducted in the close vicinity of the water wells are used for establishing empirical relationships between the hydraulic and geoelectric parameters. The transmissivity is linearly related to the transverse resistance and hydraulic conductivity is also linearly related with the average transverse resistivity, while the salinity is found to be inversely related to resistivity. These relations had been utilized in predicting the hydraulic parameters and salinity in all vertical electrical sounding sites, and a priority of drilling water wells has been presented in the study area. It can be concluded from this study that the geoelectrical sounding method can be successfully used not only for exploration of groundwater resources but also for estimating the hydraulic parameters of the aquifer. It can substantially reduce the amount of test drilling required by allowing a more intelligent selection of the well sites.



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*Source: 585243-2010-12-13.xml*