## 3 Materials and Methods  
The methodology employed in this study was based on assessing the correlation between well yield and well depth with the underlying geological formations. To achieve this, a geological map of Morocco was edited in a Geographic Information System (GIS) at a scale of 1:500,000, obtained from the Moroccan Ministry of Energy and Mines. Topographic maps were generated from a Digital Elevation Model (DEM) with a spatial resolution of 30 m, downloaded from the United States Geological Survey (USGS) website ([[http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)]([http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)), accessed on 14 December 2022). The drainage network was also derived from the DEM data (Table 1). Hydrogeological data, including well flows, the resistivity of geological formations, and groundwater piezometric levels, were extracted from borehole logs of 64 wells, obtained from the Draa-Oued Noun Hydraulic Basin Agency, and tracked from 1970 up to the present time. Furthermore, flood data were used to estimate extreme flows for sizing the future recharge dam to promote water infiltration in the alluvial aquifer. In addition, a geophysical survey was conducted in the northern part of Tata city to evaluate the recharge capacity of the alluvial deposits by the recharge dam. The survey was conducted in November 2017 using the Schlumberger configuration with a maximum current electrode spacing of 250 m, which yielded the apparent electrical resistivity (\(\rho\)a, \(\Omega\) m) at different depths of the soil. Fifteen Vertical Electrical Soundings (VES) were executed and distributed across three profiles. The Schlumberger configuration was selected due to its better resolution, greater probing depth, and less time-consuming field deployment compared to other configurations [38]. The VES electrode array recorded the electrical current I applied to the outer A and B electrodes, and the potential difference \(\Delta\)V was measured between the inner M and N electrodes [39, 40, 41]. The apparent resistivity \(\rho\)a recorded by the \begin{table}
\begin{tabular}{c c c c} \hline
**Category** & **Data Type** & **Resolution** & **Source** \\ \hline Topographical & Raster & 30 m \(\times\) 30 m & DEM ([[http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)]([http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)) (accessed on 14 December 2022)) \\ Drainage network & Raster & 30 m \(\times\) 30 m & DEM ([[http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)]([http://earthexplorer.usgs.gov/](http://earthexplorer.usgs.gov/)) (accessed on 14 December 2022)) \\ Geological & Raster & 1:500,000 & Geological map of Morocco (Ministry of Energy and Mines of Morocco) \\ Geophysical & Raster & - & - \\ Well & Vector & - & The Draa-Oued Noun Hydraulic Basin Agency (Agadir, Morocco) \\ \hline \end{tabular}
\end{table} 
Table 1: Database of the Tata basin. Figure 5: Hydrogeological functioning model of the groundwater alluvial in the Tata region. VES can be defined as per [PERSON] and [PERSON] [41], [PERSON] et al. [42], and [PERSON] and [PERSON] [43]:  
\[\rho a=K.\ \Delta V/I \tag{1}\]  
where: \(\rho a=Apparent resistivity (Ohm.m); \(\Delta V=Potential difference (mV); I = Current intensity (mA); K = Geometrical electrode factor (Equation (2)). \[K=[2\pi/(1/\Delta M-1/\Delta N-1/\Delta M+1/\Delta N)] \tag{2}\]  
The quantitative interpretation of the measurements, previously plotted on a bi-logarithmic diagram, begins with smoothing the curves. Automatic processing is then utilized to perform data inversion, allowing the geophysicist to obtain the correct model through successive approximations until the identification of geological layers. The comparison of these results with well data enables a reasonable estimation of the true resistivities.