The Adamawa Plateau, located in the Adamawa region which is one of the ten regions of Cameroon, is considered as the water tower of the country. Despite this appellation, many people lack drinking water especially in rural areas where the search for sources of reliable drinking water has become an important issue for villages in this region of Cameroon. In fact, the population growth has led to a serious shortage of drinking water, which is why the drinking water points must be exploited with the greatest care in order to avoid their exhaustion and their sustainable use. This poses a great challenge for citizens and the government [1] , who has to deal with the inadequate supply of drinking water in the region, which has become a chronic problem. In addition to the high population growth, the shortage of drinking water due to insufficient knowledge of the potential of the underground aquifer especially with respect to the characteristics of the latter, and the aggressive use of water [2] , it is also important to pay attention to the quality of the water used [3] . It is therefore very necessary to first highlight the existence of these aquifers and their hydrogeological characteristics. As a result, the integration of aquifer parameters calculated from existing drill locations and surface resistivity parameters extracted from surface electrical measurements shall be used effectively. This work, which is an application of the geoelectric prospecting method, attempts to provide a solution to the above-mentioned problem with the aim of producing a database that could be used for detailed groundwater exploration activities in the study area.

The Adamawa plateau which is the study area of this work is found in the Adamawa region of Cameroon, which is located in the heart of Central Africa between latitudes 6˚N and 8˚N and Longitudes 11˚E and 16˚E. The vegetation encountered is of shrub savanna type with the preponderance of cereal crops. Climate changes in this region where the average temperature (between 21˚C and 29˚C) increases; average annual rainfall (800 mm to 1600 mm) decreases and groundwater has increased up to 4 m in 15 years [4] . Geologically, the Adamawa plateau region of Cameroon (Figure 1) presents itself as a volcanic axis characterized by a fissured basaltic volcanism. The fault leaving Foumban, joins it and crosses away almost diagonal. It is one of the zones in Cameroon where one can meet several geological accidents.

The basement of the Adamawa plateau region consists of a Precambrian granito-gneiss complex (Figure 1) that recorded Pan-African granitization [6] . That basement is overlain by a sequence of basaltic to andesitic lavas that are largely of Tertiary age [7] . These lavas are essentially alkaline indicating an affinity to continental rifts [8] . The sedimentary formations here are mainly composed of conglomerates and marl of the Cretaceous Mbere and Djerem Troughs [7] [9] . These formations have undergone intense tectonic activity resulting in the emplacement

of basin structures which were frequently filled by volcanic material upwelling through deep fractures in the Adamawa region.

The Adamawa plateau is sometimes called the “water tower” of Cameroon, since a large number of rivers of the country have their sources in this region and experience floods from May to September during the rainy season. The rivers of the region flow into three different basins: the Niger River, Lake Chad, and the Atlantic Ocean. The hydrogeology of the region is marked by continuous alterite aquifers. In the granito-gneisses, this reservoir is generally from 1 to 20 m where it is characterized by clay dominance [10] . These aquifers overcome a cracked horizon of the granite-Gneissic basement fed by rainwater and stream beds. It constitutes the aquifer that is essentially prospecting because it concentrates most of the groundwater reserves and is supposed to be protected from seasonal fluctuations [11] . We can note the presence of wells and boreholes that are functional all year round, resulting from multiple development support programs.

The Adamawa plateau has also been the subject of a recent study that portrays the study of the hydrogeophysical characteristics of the Pan-African aquifer [12] . This study establishes unequal distribution of transmissivities by an alternative approach based on the interpretation of vertical electrical sounding data. Another study based on electrical resistivity tomography (ERT) and self-potential data was carried out at Meiganga in the Department of Mbere, in the Adamawa region [13] . This made it possible to delimit the groundwater producing areas in this locality and the resistivities of the geological formations encountered. However, these studies do not show a geophysical mapping of the aquifer and a station-by-station geoelectric study in various localities in the region. The types of data used in these studies do not make it possible to sufficiently assess the characteristics of aquifer zones throughout the region. All these aforementioned raise the need to carry out a geophysical study using a more direct method of all vertical electrical soundings conducted in the region.

The Schlumberger configuration of a linear electrodes array (AMNB) was used to locate and characterize aquifers. With this technique, whereby electrical resistivity variations are expressed as a function of depth, forty (40) Vertical Electrical Sounding (VES) have been carried out in the study area using the terrameter model SAS-300B. The operational principle rests on the fact that ground injection of current through current electrodes A and B enables the measurement of the potential drop between potential probes M and N (Figure 2). Potential electrodes M and N are kept fixed at the center of the array while current electrodes A and B are moved outward symmetrically [14] . By increasing the distance between the current electrodes from 3 to 166 m, the layer resistance ∆V/I was directly measured, and its apparent resistivity ρ_a was calculated using Ohm’s law (Equation (1)) while taking Equation (2) into consideration. Apparent resistivity depends on several factors such as true layer resistivities, their boundary, and the location of electrodes. However, lack of uniformity or split of layers can be observed.

ρ a = K V M N I A B (1)

− K (in m) is the geometric factor depending on the array of electrodes;

− V_MN: potential drop between electrodes M and N, in mV;

− I_AB: electric current injected between electrodes A and B, in mA. Where:

K = 2 π ( 1 A M − 1 B M − 1 A N + 1 B N ) (2)

The curve-matching technique was used in this study to calibrate and interprete the sounding curves [15] . Calibration was conducted with experimental boreholes drilled in the vicinity of several VES points. These experimental parameters were thereafter accurately interpreted using an inverse technique program [16] [17] . In this case, a weighted least squares inversion algorithm was used to propose geoelectrical models of the study area. The process here is done in several steps which include:

a) Importing survey data collected in the field

On the sample sheet used during the data collection, two variables were used for the modeling: the values of the spacings of AB/2 and that of apparent resistivity ρ_a. Thus using the modeling tool JOINTEM (joint interpretation of electromagnetic and geoelectrical soundings using 1-D layered earth model), more precisely in the box denoted “method by direct current”, abilogarithmic paper is employed whose abscissa takes the values of AB/2 and its ordinate takes values of ρ_a.

b) Matching curves

The inversion process involves bringing the theoretical curve so that it superimposes itself the most possible on the points of soundings. This curve has well defined parameters which are the number of layers, the resistivity of layers and the thickness or depth of the layers (Figure 3). However the overlaying of the curves can be correct but the parameters obtained do not reflect the reality, and so there will be need to change these parameters from the information available at first sight. This is in order to obtain a quadratic error average (RMS) value as small as possible and the sum of damping factors equal to one. This process was carried out taking into account several precautions, such as the precision of various

calculations, a reasonable geologic concept and the hypothesis of a one-dimensional (1D) medium [18] . The geologic conditions of the region were favorable for assuming 1D model for vertical electrical soundings data interpretation [12] .

The results of this study are from a quantitative study done with vertical electrical sounding curves summarized in a table and from a qualitative study through cartography.

The interpretation of the vertical electrical soundings made it possible to highlight the geoelectrical models of the basement of the study area. To this end, the subsoil of the study area has been subdivided into three major groups. The first is a shallow (<14 m) superficial infiltration zone dominated by laterite whose resistivity is quite high (>1000 Ω∙m) and clay (<600 Ω∙m). The second zone is a weathered zone which, in the majority of cases constitutes a superficial aquifer with a resistivity range between 81 Ω∙m and 960 Ω∙m and thickness range between 12.2 m and 26.8 m. This weathered zone overcomes a granitic horizon that presents a large variety of resistivity range (between 12 Ω∙m and 10705 Ω∙m) thus highlighting the strong heterogeneity of rock. The deep water producing areas would be around 16 m and 40 m of depth. However it could be noted that the results obtained by tomographic and Self-Potential data analysis in part of the region of Meiganga (Meying et al., 2018) revealed the presence of lateritic formations (lateritic soils, laterites) with high resistivity values (>2000 Ohm∙m), a gneissic weathered/fractured arena with low resistivity values (<850 Ohm∙m) which represents the aquifer training and the gneissic basement. As a result, the inverted resistivity models have revealed productive groundwater zones at depths of 20 to 25 m and are considered to be deeper groundwater zones with depths of about 10 to 13 m, for shallow groundwater [13] . However, some differences are observed when the results are compared, this may be due to the greater investigation area which is more extensive in the case of our study but also the type of data exploited.

In addition, a comparative study between the geophysical parameters obtained in the most recent study by inverse slope method [12] and those obtained by the least-squares inversion has been carried out and shows by Table 2.

This table shows that the parameters of the aquifer are almost similar with both approaches. Therefore, the results obtained are in agreement with those of Arétouyap et al. (2018).

Alteration is an important factor in the search for groundwater, because the weathered layers are very porous and weakly permeable due to the presence of clay. Weathered layers are known to have a very good water storage function [21] . The stations of great hydrogeological interest are S.2, S.4, S.11, S.13, S.17, S18, S19, S.23, S.25, S.26, S.29, S.30, S.33 and S.37 because they have weathered and fractured formations of great thicknesses On the other hand, the weathered layers are weak thicknesses and almost non-existent in some stations like S.3, S.12, S.16, S20, S.28, S.31, S.32, S.38, S.39 and S.40.

The interpretation carried out on vertical electrical sounding curves corroborate with lithological data from boreholes in the area.