This study focuses on the Sissili sub-basin, located in Burkina Faso ( Figure 1 ) shaped like a triangle, it covers an area of 7559 km². The sub-catchment hydrology is strongly influenced by the altimetry ranging between 281 - 451 m. The Sissili River flows across a relatively monotonous plateau, with little relief and a slight incline from north to south: the river’s course which is oriented North-South between Thyou and Tabou, becomes North-West-South-East between Tabou and the Ghana border. From a morphological point of view, the Sissili watershed can be divided into two distinct sections: a northern part with little contrasting relief with abundant lateritic cuirasses hiding a bedrock that only rarely outcrops; a second part in the southern section with decapitated cuirasses leaving only witness mounds with numerous granite domes. This phenomenon is attributed to the regressive erosion of the river [18] . The sub-catchment encountered formations display geological diversity and can be classified into two primary geological groups from the Proterozoic era: the plutonic and the sedimentary volcano group. The aquifer system is typically developed within a weathered and fractured basement context. It is composed of three primary layers: a superficial lateritic cover, an intermediate saprolite zone and a deeper fissured that extends to the basement. Climatically, the region experiences two (2) distinct seasons: a dry season from November to April and a rainy season from May to October. The Sissili sub-basin has two climates: a Sudanian-type climate (southern Sudanian) located south of parallel 11˚30'N and a northern Sudanian-type climate. Annual precipitation averages over 900 mm, with a rainy season that lasts more than 6 months of the year ( Figure 2 ). However, rainfall has been on a decreasing trend over the last two decades and there are slight fluctuations in annual temperatures [19] . The temperature has an average of 28˚C ( Figure 3 ), with highest temperature occurring between March and April.

Several authors such as [20] - [23] have highlighted the key parameters best suited for delineating groundwater potential zones in a crystalline context. Numerous studies and research findings have also identified parameters that provide a comprehensive understanding of drilling productivity in a crystalline context in Burkina Faso [18] [24] . Based on the previous research, a detailed analysis was carried out on various variables, to identify groundwater potential zones in the sub-basin. These variables were derived from a combination of Remote Sensing data, topographic maps, and borehole information. Nine (9) key variables were considered including lithology, geology, lineament density, soil type, drainage density, borehole depth, land use patterns, Topographic Wetness Index (TWI), and efficient seepage. This integrated approach aims to offer a comprehension understanding of groundwater dynamics within the Sissili sub-catchment by employing tools such as ArcGIS, QGIS and R. ArcGIS and QGIS software were used for spatial data compilation, analysis, and visualization, while R was used for ANN models building and validation. Also, a total of 256 boreholes were selected based on the availability of reliable data, such as verified geographic coordinates and discharge values. A 5 × 5 km grid was applied over the study area to ensure a spatially balanced distribution covering the different lithological and hydrological zones of the sub-basin. In each grid cell containing data, a representative borehole was retained. This integrated methodology allowed both an assessment of spatial heterogeneity and the consideration of practical constraints related to data availability. Data from various sources were collected, processed, and integrated to delineate the GWPZs. Table 1 resumes all the data sources and resolutions.

The identification of groundwater potential areas in the sub-basin is carried out by taking into account the main factors (parameters) influencing the recharge process and groundwater occurrence. They were selected based on an extensive literature assessment and for their direct impact on groundwater presence, replenishment, storage, and flow. Each factor affects groundwater potential by exerting differing degrees of influence.

Lithology: The occurrence and flow of groundwater are significantly influenced by the type of rocks, their structural characteristics, and their hydrological properties [11] .

Geology: Geology affects the groundwater recharge by controlling the percolation of water [10] . Following rasterization, the data were categorized into eight (8) geological classes and five (5) lithological classes.

Efficient seepage: Rainfall is an essential factor in defining groundwater potential zones. It is, in fact, the primary source of natural recharge that develops groundwater resources [25] . CHIRPS satellite rainfall data for the year 2023 were used in this study, due to the strong correlation (85%) between CHIRPS data and observed rainfall data, and the limited availability of observational data in the study area. The Thornthwaite method has been applied in Excel to estimate the seepage water, which represents the portion of rainfall that infiltrates the subsurface and contributes to groundwater recharge. The efficient seepage is calculated based on climatic parameters and the usable ground reserve (RFU), using the Equation (1) below:

Q_seep = P − Q_R − AET−RFU (1)

Where Q_seep represents the rainfall seepage water, Q_R is surface runoff, P the precipitation, AET is actual evapotranspiration, and RFU refers to the usable water in the ground, sourced from BUNASOLS (Source: Thornthwaite method).

Lineament density: The lineaments were extracted by multi-software processing of ALOS PALSAR data through firstly principal component analysis (PCA), followed by application of directional filter SOBEL on 0, 45, 90, and 135 degrees. Then manual lineament extraction has been processed. The lineaments have then been validated on the field. A lineament density (km/km²) map has been prepared using the line density tool of spatial analysis tool of QGIS software, following the Equation (2) below:

$\text{D}f=\frac{{{\displaystyle \sum }}_{i=1}^n{\text{L}}_i}{\text{A}}$ (2)

Df = lineament density [km/km²]; L_i = total length of lineament in km,

A = Area occupied by fractures in km².

Drainage density: Drainage density is the total length of the river system per unit of watershed area [26] . Using the ArcHydro tool of ArcGIS, individual drainage networks were extracted and delineated from the derived Digital Elevation Model (DEM) ALOS PALSAR . The equation (3) below allows the computing of the drainage density value in km/km².

$\text{D}d=\frac{{{\displaystyle \sum }}_{i=1}^n{L}_i}{A}$ (3)

Dd = drainage density [km/km²]; Li = total length of the drainage network in km; A = Area considered in km².

Land use/land cover (LULC): LULC plays a crucial role in groundwater recharge [11] . The Land Use/Land Cover (LULC) map has been derived from ESAWORL ( https://esa-worldcover.org/en ) and has a resolution of 10 m × 10 m.

Soil: The medium through which water must penetrate to reach the water table is soil, which is an important factor in groundwater recharge and discharge [27] . The country soil data available is collected from BUNASOLS.

Borehole depth: The shallow depth indicates the high-water table inside the area while a deep depth represents challenges in terms of accessing its water resources [28] .

Topographic Wetness Index (TWI): The Topographic Wetness Index (TWI) serves as a valuable tool for identifying groundwater potential through the analysis of spatial variations in soil moisture [20] . The calculation of TWI is based on the following Equation (4):

$\text{TWI}=\ln \frac{\alpha }{\tan \beta }$ (4)

where $\alpha$ is Upslope contributing area and β Topographic gradient (Slope).

Borehole yield: The high value of borehole yield indicates that the area has favorable hydrogeological conditions for groundwater exploitation [28] . This parameter will serve to validate the different results obtained.

The impact of various factors on the productivity of boreholes was assessed using weighted values, with the weighting approach based on expert opinions used in previous work [29] [30] carried out in the basement region. The scores from previous studies were used to assign weights to the factors in the current study. A common interval of 1 to 10 is used where the most favourable class for groundwater potential was assigned a score of 10, and the least favourable class was given a score of 1 based on [31] scale during the comparison between the parameters selected. The various factors were then compared pair-wise to create square matrices, from which the weighting coefficients were derived using the eigenvectors of these factors. The approach described by [32] was employed in this investigation. To reduce the subjectivity all parameters were normalized and reclassified., as they were measured on different scales and units. The pair-wise comparison establishes the relative importance of each factor by comparing them two at a time. [14] demonstrate that a layer, with a high-weight parameter, can greatly affect the groundwater potential while a layer, with a low-weight parameter tends to have only a minor impact. The relative comparison importance of each parameter was determined using Saaty’s scale as shown in Table 2 .

All the thematic maps were integrated using the ArcGIS spatial analysis tool (Weighted Overlay Index (WOI) method) to generate a map depicting the groundwater potential zone. The final weights for all parameters were determined through the following steps using the following Equations (5)-(10).

1) The sum of the values in each column of the pair-wise comparison matrix:

${\text{L}}_{ij=}\underset{i=1}{\overset{n}{{\displaystyle \sum }}}{C}_{ij}$ (5)

Where, L_ij is the total column value of the pair-wise comparison matrix and C_ij is the criteria used for analysis, such as drainage density, elevation and slope.

2) Normalized pair-wise comparison matrix:

${\text{X}}_{ij}=\frac{{\text{C}}_{ij}}{{{\displaystyle \sum }}_{n=1}^n{\text{C}}_{ij}}$ (6)

X_ij represents the normalized pair-wise comparison matrix.

3) Standard Weight:

${\text{W}}_{ij}=\frac{{{\displaystyle \sum }}_{j=1}^n{\text{X}}_{ij}}{\text{N}}$ (7)

W_ij = Standard Weight and N = number of criteria/parameters.

4) Consistency vector values:

$\lambda =\underset{i=1}{\overset{n}{{\displaystyle \sum }}}{\text{CV}}_{ij}$ (8)

Where λ is the Consistency vector.

5) The Consistency Index (CI) used as a degree of consistency:

$\text{CI}=\frac{\lambda -n}{n-1}$ (9)

where CI = Consistency Index and n = Number of criteria.

6) Consistency ratio (Cr):

$\text{C}r=\frac{\text{CI}}{\text{RI}}$ (10)

RI = Random Inconsistency (summarizes in Table 3 ). If the Consistency ratio is less than or equal to 0.10, then, the inconsistency is acceptable.

The Artificial Neural Networks (ANN) are among the most commonly employed methods in machine learning algorithms [33] [34] and their application in water resources management, utilization, and modelling is increasingly common [35] . ANNs are beneficial because they can model complex data relationships, allowing the network to generalize and make predictions on new inputs without assuming a specific data distribution [36] . In this study, the ANN model was built using R software scripts. The process of using ANN for groundwater potential mapping involves several key stages. The design and configuration of the ANN model involve the inclusion of a suitable number of inputs, hidden and output layers. In the initial stages, groundwater potential parameters (data) have been obtained from a variety of sources, and for the current study, the same parameters selected for the multicriteria analysis have been used. All in all, 256 boreholes locations were used. The collected data have been then pre-processed to detect and correct any inconsistencies or errors that may have occurred. Then, the pre-processed data were randomly partitioned, seventy-five per cent (75%) into training while the remaining twenty-five per cent (25%) into testing datasets. The former is used to set or calibrate the ANN model and the latter to validate (test) its accuracy. As a dependent variable, the borehole yield was reclassified for the study area using scientific and objective criteria suggested by the Comité Interafricain d’Etudes Hydrauliques (CIEH). Groundwater suitable area training dataset was made up for areas where borehole yield was greater than 2.5 m³/h, and a non-suitable area dataset was built up for areas where borehole yield was less than 2.5 m³/h. The zonal statistics mean tool in QGIS was employed to compute the average value of a parameter within designated zones. This study utilized borehole yield locations as sites to derive the average values of nine (09) important parameters: lithology, geology, lineament density, soil type, drainage density, borehole depth, land use patterns, Topographic Wetness Index, and effective seepage. This approach allowed the evaluation of spatial distribution and relationships of these elements. The chosen neural network (NN) structure is a Multi-Layer Perceptron (MLP) that comprises three layers. The initial layer served as the input layer, with its nodes representing thematic maps of the nine (9) parameters influencing groundwater conditions in the Sissili catchment area. The second layer corresponds to the internal or “hidden” layer with five (5) nodes, while the third layer functions as the output layer, responsible for presenting the output data with one (1) output node. This output data contains information regarding groundwater potential areas, which serve as the training sites for the model. Within the hidden layer, every node is interconnected with nodes in both the preceding and following layers through weighted connections. The architecture of the Artificial Neural Network (ANN) was optimized through manual hyperparameter tuning and cross-validation. Using the back-propagation training algorithm, the weights of each factor can be determined through the method defined by [37] . The backpropagation algorithm optimizes its weights and biases, to minimize the disparity between the predicted and actual groundwater potential values. It can incorporate multiple hidden layers, which empower the network to conduct various levels of processing and computation. Subsequently, the validated ANN model has been employed to generate the groundwater potential zone map. The area under the Receiver Operating Characteristic (ROC) and the Area Under Curve (AUC), which are generally used as statistical criteria for validating machine learning models were used to evaluate the predictive capability of the proposed model [38] .

The nine (9) parameters selected such as Topographic Wetness Index, geology, effective seepage, lithology, lineament density, soil type, land use/land cover patterns, drainage density and borehole depth to delineate GWPZs were mapped and analyzed as described in the following Figures 4-13 .

Geology affects the groundwater recharge by controlling the percolation of water flow [10] . The geological map of the study area displays eight distinct geological units, primarily consisting of tonalite and granite, which are conducive to infiltration ( Figure 4 ). Tonalite, with low potentiality is widely represented and centred in the sub-basin, while the basalt with very low groundwater potential is less important in the sub-basin.

Figure 5 describes the lithology of Sissili sub-catchment which is obtained from the BUMIGEB. The dominant lithologies observed are the migmatitic and anatectic gneiss which are not favourable for groundwater infiltration. The lithology with moderate groundwater potential, less represented in the sub-basin, is paragneiss.

The term “lineament” refers to the linear elements of a landscape visible in satellite and aerial photography, mostly having a geological origin [26] . Figure 6 presents the lineament density map and reveals a prevalence of moderate lineament density, characterized by values ranging from 0.032 to 1.79 km/km². High lineament density is favourable to infiltration while the low lineament doesn’t favour water infiltration.

The drainage density is an inverse function of permeability. An area with a low permeable surface tends to have high drainage density. As a result, high drainage density implies low groundwater potential [25] . The resulting map illustrates in Figure 7 , four major density classes ranging from 0 - 1.6 km/km², with high densities around rivers and at tributary crossings, decreasing as one moves away from rivers.

Figure 8 represents the efficient seepage map in the sub-basin, ranging from 37 - 70 mm. The efficient seepage contributes to the recharge of aquatic environments and water tables. This is assumed to be the amount of rainfall that penetrates the aquifer. The southern part of the Sissili sub-catchment is the region with the highest infiltration portion.

The various forms of land use patterns that have been identified ( Figure 9 ) in the sub-basin are primarily trees, grass, agricultural land, crops, and built-up. As the sub-basin is located in a predominantly rural area, the main land use is agricultural (crop) which has a low water infiltration. The built-up constructions also decrease water infiltration, whereas vegetation and water bodies increase water penetration into aquifers through the confinement of water in the soil, thus avoiding direct evaporation [39] .

The depth of the boreholes is presented in Figure 10 with values ranging from 35 to 99 m. This range indicates that majority of the boreholes have been realized based on deep depth which is synonymous with limited groundwater availability. This result shows that mainly areas close to the southern Ghanaian border are favourable to water infiltration (shallow depths).

The Topographic Wetness Index (TWI) values obtained are ranked between 7.3 and 26.32 as presented in Figure 11 . Greater TWI values correspond to reduced slopes, thereby facilitating a greater potential for groundwater accumulation.

The soil map obtained in Figure 12 classifies the three main soil categories into hydromorphic, raw mineral, and poorly developed soils. Each class is characterized by its role in groundwater accumulation. Raw mineral and poorly developed soils are present in relatively small areas and it is highly resistant to recharge because of its low permeability.

The different selected parameters have been reclassified, and each parameter class have been allocated a weigh and a normalized weight to prepare the groundwater potential map. The following Table 4 summarizes the criteria and sub-criteria ranges.

Table 5 presented below displays the normalized pair-wise matrix assigned to each thematic layer throughout the process of pair-wise comparison. A square matrix was utilized to conduct a pair-wise comparison of all input parameters, with the diagonal components consistently set to 1. The calculation of the normalized pair-wise matrix using Equation (6).

The output from the AHP final map obtained was classified into areas of very low, low, moderate, high, and very high groundwater potential zones. The results were validated using the borehole yield data collected. Figure 13 gives the final map of the groundwater potential zones obtained.

The final map of the ANN process was categorized into zones of very low, low, moderate, high, and very high groundwater potential. The results were corroborated using the yield data from the drilled wells, as well as the AUC and ROC obtained post-analysis. Figure 14 represents the groundwater potential zone map obtained.

The verification of the reliability of a model’s output is necessary before utilizing the obtained results. Consequently, yield data from seventy-eight (78) existing boreholes were used to validate the delineated GWPZs ranging from 0.51 to 12.9 m³/h, with an average of 2.55 m³/h. To assess the degree of accuracy of the AHP process, the Consistency Index (CI) and the Consistency ratio (Cr) have been calculated based on the previous equations (9) and (10). The Eigenvector technique was used to calculate the principal Eigenvalue (λ) through the formula (8) where λ_max = 9.56. The Cr = 0.048, which is less than or equal to 0.10, showing that the inconsistency is acceptable. As a result, boreholes situated in areas with very low exhibit a yield ranging between 1 - 2 m³/h, and low groundwater potential exhibits a yield ranging between 2.1 - 5 m³/h. boreholes located in areas with moderate groundwater potential exhibit a yield ranging from 5.1 to 10 m³/h, while those in high and very high groundwater potential zones demonstrate yield superior to 10 m³/h following the Comité Interafricain d’Etudes Hydrauliques (CIEH) classification. The AHP result shows 18% of boreholes fall within the very low groundwater potential zones while 29% of boreholes on the ANN map. In the low potential zone, 27% of boreholes lay in this class in AHP map while 16% of boreholes in ANN map. In the moderate potential zone maps obtained with AHP and ANN process, respectively 32% and 18% of boreholes are located in this class, while in the high potential zone class 15% and 22% of borehole, respectively are identified in this class. Finally, the very high groundwater potential class accounts

for 8% and 15% of boreholes in the AHP and ANN maps, respectively. Also, the Area Under Curve (AUC) has been calculated, generally used as statistical criteria for validating machine learning models to evaluate the predictive capability of the model. The ROC is quantitatively characterized by the AUC. In an ideal classifier (perfect model), the AUC equals 1, whereas for a random classifier (inaccurate model), it yields a value of 0.5 [40] . Figure 15 displays the AUC of 0.87 while Figure 16 shows the satisfactory performance result of 0.93.