## 4 Results and Discussion
### Impact of the Structural Context on Hydrogeological Potential
\begin{table}
\begin{tabular}{c c c c c c c c} \hline \hline
**Borehole** & **X** & **Y** & **Total Depth** & \begin{tabular}{c} **Lithological** \\ **Formation** \\ \end{tabular} & \
\begin{tabular}{c} **\% of the Cumul** \\ **Length Fractured** \\ **Formation** \\ \end{tabular} &
\begin{tabular}{c} **Yield of Borehole** \\ **(L/s)** \\ \end{tabular} & **Permeability** \\ \hline S1 & 40,767 & 274,334 & 80 & Gd & 12\% & 0.05 & - \\ \hline S2 & 41,381 & 274,956 & 32 & Gr & 60\% & 3.5 & \(5.32\times 10^{-8}\) \\ \hline S3 & 41,192 & 273,889 & 32 & Gr & 66\% & 0.5 & \(1.18\times 10^{-7}\) \\ \hline S4 & 41,107 & 273,605 & 42 & Gr & 36\% & 1.8 & \(1.04\times 10^{-6}\) \\ \hline S5 & 40,292 & 270,074 & 80 & Gd & 26\% & 0.08 & - \\ \hline S6 & 40,209 & 270,323 & 60 & Gd & 16\% & 0.02 & \(1.27\times 10^{-6}\) \\ \hline S7 & 39,667 & 271,138 & 50 & Gd & 20\% & - & - \\ \hline S8 & 41,829 & 271,506 & 80 & G & 32\% & 0.55 & \(1.07\times 10^{-7}\) \\ \hline S9 & 40,528 & 271,663 & 50 & Gd & 14\% & 0.6 & \(4.3\times 10^{-7}\) \\ \hline S10 & 40,998 & 271,739 & 80 & Gd & 25\% & 0.45 & \(0.95\times 10^{-7}\) \\ \hline S11 & 41,356 & 270,658 & 80 & G & 55\% & 1.4 & - \\ \hline S12 & 40,710 & 271,121 & 50 & G & 14\% & 0.06 & - \\ \hline S13 & 40,643 & 273,948 & 80 & Gd & 25\% & 0.3 & \(0.9\times 10^{-7}\) \\ \hline S14 & 39,380 & 273,811 & 60 & Gd & 12\% & 0.02 & - \\ \hline S15 & 39,784 & 273,385 & 80 & Gd & 0\% & - & - \\ \hline \hline \end{tabular}
\end{table} 
Table 1: Hydro-structural characteristics of the 15 boreholes drilled in the granitic basement of Ifni [8; 87]. The newly created structural map (Figure 9), was used to measure the distances between the positive water wells and the tectonic faults. The analysis revealed that 35.24% of these wells are located within 100 m, while 21.23% are located between 100 and 200 m. Furthermore, 26.85% of the wells are located between 200 and 400 m, and only 16.68% are located beyond 400 m (Figure 12). These results demonstrate a strong and significant correlation between the presence of positive water points and the proximity of faults and tectonic nodes. Therefore, it is evident that these structures have a significant impact on groundwater flow and aquifer recharge in the study area. To confirm the impact of faults on groundwater potential in the study area, the high-resolution (7200 Hz) electrical resistivity map, although covering a small area (Larb a Misti) compared to the gravity data, was used (Figure 13). The relatively high frequency of 7200 Hz was used for shallow subsurface imaging with a penetration depth of 84 to 187 m (Table 2). The negative boreholes (S16 to 21) are located in high resistivity ranges (1024 Ohm.m) corresponding to sound basement formations without fault crossings. On the other hand, the positive boreholes (S1 to S15) are located in anomalies of low linear resistivity reflecting the impact of fault crossings, which, thanks to the water they drain, tend to decrease the  
Figure 11: Location of reconnaissance boreholes (S1 to S15). resistivity values of the formations. Resistivity data can provide valuable information for mapping and identifying potential groundwater zones by helping to identify sub-surface areas and geological features that may influence the movement and availability of groundwater. Figure 12: Section of decrease in percentages of positive water points as a function of distance to fractures and nodes in the lfni inlier. Figure 13: Spatial distribution of apparent resistivity anomalies in the Larb a Misti area superposed by faults and water boreholes (S1 to S15).