The geology of the southern part of Mali is characterized by Precambrian basement rocks of the West-African craton which are comprised of the Man (south) and Reguibat (north) shields, and significantly smaller inliers of Kenieba and Kayes. These exposed basements blocks are bounded and separated by Pan-African fold belts and Late Proterozoic to Phanerozoic sedimentary basins, including the expansive Taoudeni basin. The Man shield is subdivided into three main lithostratigraphic units: The Liberian shield of Archean age, and the Birimian and Tarkwaian, which are considered to be Early Proterozoic [6] [7] .

Moreover, the geology of the southern part of Mali is made up of a volcano-sedimentary sequence of Birimian rocks, tightly folded, but weakly metamorphosed during the Eburnean orogeny (2.1 Ga) and intruded by syn-to late-tectonic granites (Figure 1). The Birimian rocks comprise a series of fine-grained sedimentary and volcanic rocks. The sedimentary sequence consists of meta-arenite, meta-argillite, meta-greywacke and meta-carbonates. The volcanic formations are comprised of andesite tuffs, basalts, and dacites rocks with mafic components predominating.

Southern Mali is bound on to the north and east by the Taoudeni Basin comprising Upper Mid- to Late-Proterozoic sandstones and interbedded pebble conglomerates of the Taoudeni basin (often termed the Infra-Cambrian), that unconformably overlie the Birimian rocks. Both the sedimentary and volcanic sequences are cross-cut by dolerite, diorite, and keratophyre dikes. The geological setting of the Yanfolila concession area has been previously mapped and described by [8] [9] [10] [11] .

The Bale Gold province, which hosts the Kalana and Kodieran gold deposits, is located in a north-south trending anticline around 150 km long and 40 km wide which is intersected by three fault systems [12] . This structure covers an area of 6000 km², including the Yanfolila zone.

The north-northeast trending Banifing fault is the largest fault in southern Mali and is believed to have a left-lateral relative displacement with many sub-parallel shears. This fault has been traced for a strike length of more than 500 km. The faulting is accompanied by gold-bearing quartz veins and veinlets with, four principal attitudes that can range from several mm to several meters in width. The first three vein systems carry the gold mineralization.

Interpretation Map summarizes the relationship between the geological formation boundary and the mineralization index of gold and the source of location (Figure 4).

The use of existing geological data to test the work was done inside; here we illustrate some typical structures in the study area.

The effect of structures affects different levels of mineralization in the study area. Some faults are relatively small scale, widely distributed, and configured for various levels of influence on gold mineralization (Figure 4). The banifing fault (F1) system is the factor controlling the mineralization process in the region and plays on the impact of training of mineralization rocks.

Depending on the spatial distribution of the alteration anomaly and the degree of intensity of the alteration force, the information on the alteration of iron is closely related to the mineralization of rocks/process. As field relationships and micro-textural data indicate that the primary gold mineralization is shear hosted.

The high gold anomaly value is limited to the west and south, where gold values are low in breastplates and alluvial soils. The geochemical anomalies associated

with the mineralization are controlled by the fault system. The degree of development of the lineaments and the overall interpretation of their spatial distribution reflects the structural setting of the study area. The results showed that the advantages of the orientation of regional lineaments to NE. While field relationships and micro-textural data indicate that the primary gold mineralization is shear hosted [13] . In Hoggar, gold mineralization depends on a double control, first order giant sub-meridian shear zone control and the gold districts disposed in N40 -50 E corridors that may be interpreted as extensional [14] .

In this work the Banifing fault (F1) is the biggest fault, and supposed to have a relative moving in left-side with lots of sub-parallel shears. Clearly noticed that this fault on remote sensing maps. In southern Mali, the other north trends structures are considered co-genetics Banifing fault system. The gold occurrences are spatially controlled by the system of NNW and NNE trending faults. Both trends structures could also be interpreted in terms of structural corridors Banifing. While Gold deposits in the Syama and Tabakoroni goldfields in southern Mali occur along a north-northeast trending mineralized litho-structural corridor that trends for approximately 40 km [15] .

The granite massif lying north several kilometers in length (Figure 5). This granite massif contains orthogneisses diorite rocks and monzonitic. It is considered a syn-tectonic intrusion often associated with hornfels, amphibolite quality contact metasomatic and local migmatization.

Small groups of diorite, granodiorite and porphyry plagiogranite also infringe the volcano-sedimentary sequence. These types of rocks are located at the intersection of the northwest and north-east fault (Figure 5). In general, the intrusive rocks of the region have a spatial affinity, combining them with local structures is considered particularly important in the location of the all the main gold deposits in southern Mali. However, the Tellem gold prospect is hosted by intrusive rocks of diorite to porphyry dacitic composition that crosscut the pyroclastic and black shale formation [16] . In the Oudalan-Gorouol, Gold mineralization

is sited along five northwest-trending metallogenic corridors, specifically, where northeast-trending faults and shears crosscut or coalesce with northwest-trending thrustfolds [17] . The creation of a deep laterite weathering profile and supergene enrichment of the residuum probably took place during the mid-Cretaceous-early Tertiary [18] .

The integrated interpretation map from the combination of the different maps, referring to the geological information in association with the gold content greater than 2 g/t, allowed delimiting target by ArcGIS 10.2.1. The findings show two targets delineated in the study area. In the study area, two targets have been delineated.

In Solona (target 1), this zone is associated with geological structures. The contours of this zone coincide with igneous rock, which has been encountered as a highly altered material. Clay (kaolin) and ferric iron are the main alterations of the mineralized zone. On the interpretation map, target 2 is located in the center of Yanfolila area, and it is less important than target 1.

In The Yanfolila study area, Mineralization is associated with well-developed NNE and ENE structures. The presence of diorite intrusions approximately mineral showings, Quartz-sulphide vein, and veinlet develop with associated gold values.

The integrated interpretation indicates several gold anomalies coincide with broad areas. The general distribution number of lower-intensity gold anomalies within the study area. While in the Loulo-Gounkoto complex these findings demonstrate the widespread if heterogeneously distributed, nature of fluid mixing as an ore-forming process [19] . On the interpretation map (Figure 5), the delimitation of the target 1is located in the locality of SOLONA.

Clay (kaolin) and ferric iron (Fe.) are the main alterations of the mineralized zone. The presence of crates observed in oxidized meta-sedimentation indicates a probable sulfide (SO₄) mineralization. The results of the sample also confirmed that the Solona mineralization, which is believed to be controlled by NE structures intersected by secondary E-W structures.

The Solona area is mainly characterized by volcano sedimentary formations composed of slightly metamorphosed fine-grained sandstone, argillite, and siltstone.