Petro-Structural Study of the Paleoproterozoic Formations of the Faboula Gold Deposit (Bougouni-Kékoro Basin, Leo-Man Shield)

Recent petro-structural investigations on the Faboula gold deposit located in the Bougouni-Kékoro basin, in southern Mali, north-west of the Leo-Man Shield, have provided new data on the nature and spatial organization of the lithostratigraphic units as well as their deformation style. The deposit is covered by a thick lateritic layer and is hosted by a metavolcano-sedimentary sequence of Paleoproterozoic age intersected by intrusive bodies and filled fractures of various shapes and types. The lithostratigraphic units consist of metagreywackes, metasiltstones, meta-argillites, slates and schists. Metagreywackes and metasiltstones are generally feldspathic, both may contain biotite and locally amphibole, just as slates may contain andalusite which is locally stretched. Plutonic units most often occur as stocks or as dikes on the drill core, up to 1 m. The metavolcano-sedimentary rocks are schistose and deformed under greenschist facies conditions, and locally they reach the epidote-amphibolite facies. The structural study revealed that the deposit is affected by several stages of deformation evolving from a ductile type to a brittle type via a ductile-brittle type. The dominant ductile and brittle-ductile deformations show a combination of isoclinal folding and strike-slip faults. Both the isoclinal folding and the strike-slip faults whose sigmoidal en-echelon tension gashes indicate a dextral movement in the NNE-SSW direction are the result of the same ENE-WSW regional shortening. Consequently, they highlight a transpressive deformation. This deformation noted here D2Fb, could be equivalent to the regional D2 or D3 deformations identified at the scale of the Leo-Man Shield if we refer to the style of deformation. There is an abundance How to cite this paper: Wane, O., Ouologuem, A.B., N’diaye, I., Dao, O. and Yossi, M. (2021) Petro-Structural Study of the Paleoproterozoic Formations of the Faboula Gold Deposit (Bougouni-Kékoro Basin, Leo-Man Shield). Open Journal of Geology, 11, 105-141. https://doi.org/10.4236/ojg.2021.114007 Received: March 10, 2021 Accepted: April 23, 2021 Published: April 26, 2021 Copyright © 2021 by author(s) and Scientific Research Publishing Inc. This work is licensed under the Creative Commons Attribution International License (CC BY 4.0). http://creativecommons.org/licenses/by/4.0/


Introduction
West Africa Craton (WAC) has become the target of gold exploration and exploitation by the major global mining companies because of its world-class gold deposit and the increase of the price of the precious metal.
This interest triggered the development of a lot of scientific research and industrial projects among national geological surveys, mining companies and universities for a better understanding of the geological evolution of the WAC. The interest also allowed the discovery of numerous gold deposits and the detection of areas of high-potential gold mineralization. Gold deposits in the WAC are principally hosted in the Paleoproterozoic formations, also known as Birimian formations, which developed between ca. 2312 -2060 Ma according to the integration of the previous works of many authors [1]- [16]. Many gold deposits have also been found in land of similar age in Australia, Canada, China, etc. Half of the world's gold reserves are in the Precambrian formations [17].
Mali is renowned for its wealth in gold, at least since the Middle Age [18]. In 1433 the pilgrimage to Mecca of the famous emperor Kankou Moussa helped to amplify this reality. However, the country only became an industrial exporter of this ore very recently, in the mid-1980s with the exploitation of the Kalana gold deposit. Since then, gold mining has experienced a boom, favoured by the installation of many mining companies. Nowadays, thirteen modern mines have emerged in Mali, seven in the west of the country and six in its southern counterpart including the Faboula gold deposit (FGD).
The economic importance taken by gold in recent years has pushed mining companies to leap into new research opportunities on gold and beyond all the mineral resources present in the Birimian of Mali. Projects combining both the establishment of geological maps and the prospecting of natural substances have been carried out. They led the country to rank Third African Gold Producer after South Africa and Ghana in less than a decade. The gold reserves are estimated at over 800 tons [19] and its production was 2.14 Moz (60.7 t) in 2018. It leads export product ahead of the cotton and the cattle breeding. The contribution of the mining sector in Mali's export is around 63.3% and its apport in the GDP is roughly 6.6%. In 2017 Gold production gave Mali a total of 405.30 million USD [19]. Paradoxically, the geology of the Birimian of Mali is still un-  [26]. (c) Simplified geological map of the Leo-Man Shield, after [66], with localization of study area (black circle).
Shield in its southeastern parts are covered respectively by the Paleozoic basin of Tindouf and the Neoproterozoic basin of Volta [22] [24] [25]. Liberia, southeastern Guinea and a small part of the western of Ivory Coast. It is constituted by the association of greenstone belts and granitoids [24] [26] [27] [28] [29]. It is made up of migmatites, charnockites, orthogneiss, paragneiss, banded iron formations (BIFs) and metamorphosed formations represented by amphibolites and granulites [22] [27]- [34]. According to these authors the Archean rocks underwent meso to catazonal metamorphism and were migmatized more or less locally.
The Archean domain was modelled by two tectono-magmatic events: the Leonian (~3244 -2900 Ma) and the Liberian (~2900 -2700 Ma) [24] [27] [29] [35]. An earliest evidence for continental accretion of Archean age (3542 ± 13 Ma) in the Leo-Man Shield has been recognized in Guinea on the basis of zircon dating [29]. This result has been confirmed by [34], who obtained a Nd model  [36] [37] and considered as supracrustal rocks. They were emplaced between ca. 2255 -2060 Ma according to the integration of the previous works of many authors [2] [3] [5] [6] [8] [9] [10] [11] [15] [16] [38]. The greenstone belts are slimmed and oriented curvilinear entities made up of various volcanic rocks and subordinate detrital rocks. They were principally deposited between ca. 2250 and 2180 Ma, however their formation continued until about ca. 2100 Ma [11]. They are represented by lavas, volcanoclastic and siliciclastic rocks. The lavas have a variable chemical composition ranging from basalt to rhyolite with a tholeiitic or calc-alkaline affinity [1] [2] [3] [4] [39]- [44]. The volcanoclastic and siliciclastic rocks are represented by greywackes, shales, and sandstones (flysch-type) and locally by molassic deposit (conglomerates, feldspathic sandstones, and minor argillites). According to [16] they display a NE-SW to N-S orientation in the eastern and central Baoulé-Mossi domain, while in its west part they are oriented N-S to NW-SE. Several authors noted that their emplacement indicates diachronously volcanic activities from east to the west with the oldest volcanogenic rocks preserved in the eastern part of the Baoulé-Mossi domain and the youngest in its western part [6] [16] [44].
Volcano-sedimentary basins are the deposition environments of flysches in which intercalations of subordinate lavas and volcaniclastic rocks are found. They are made up of greywackes, siltstones, argillites, schists, lavas, volcaniclastic rocks and occasionally manganiferous, carbonate and/or siliceous chemical rocks. Carbonate rocks are found mainly in the Siguiri basin and Kédougou-Kéniéba inlier [38] [45] [46] [47] [48] [49]. As well as the volcanic activities, the sedimentary sequences show similar migration from east to west. Maximum depositional ages are in the range of 2160 to 2130 Ma in the east and 2110 -2065 Ma in the west [16].
The granitoids are abundant throughout the Baoulé-Mossi Domain. They are closely associated with the supracrustal rocks. They display various mineralogical and geochemical compositions as well as geochronological characteristics and diverse settings. They are represented principally by tonalite, trondhjemite, granodiorite (TTG), gneisses, diorites and granites.  [62]. The record of basic to acidic volcanism, flysch-type sedimentation, and subsequent compressional deformation, uplift and molasse formation preserved in the Birimian Group resembles a complete Phanerozoic orogenic cycle [63].
In the Malian part of the Baoulé-Mossi domain, the geology is quite poorly constrained due to the limited outcrops and the lack of drilling in certain areas.
According to [64], there are three main basins and two principal volcanic greenstone belts ( Figure 2

Local Geological Setting of the Faboula Gold Deposit
The FGD is located in southern Mali, at the limit of the western edge of the Bougouni-Kékoro basin, not far from the Yanfolila greenstone belt and near the Kalana gold deposit (Figure 2 and Figure 3). The basin hosts a spectacular swarm of spodumene bearing pegmatites. The lithostratigraphic units of the basin contain flysch type unit, basic and acid volcano-sedimentary rocks [67] [68] [69]. They are principally represented by metagreywackes and metavolcano-sedimentary formations, and the former is topped by the latter. The metagreywackes formations are volcano-sedimentary deposits most often of intermediate composition; they are formed by conglomerates, arkoses interbedded with pyroclastic and lavas flow, most often andesitic in composition. The metavolcano-sedimentary formations include dominant flyschoid formation constituted mainly by fine-grained sediments, siltstones and argillites, which are intercalated with feldspathic sandstone. Volcano-sedimentary deposits, basic at the base and acidic upwards, are intercalated in the flysch-unit [67].
The volcano-sedimentary rocks are deformed and metamorphosed generally into greenschist facies. They have been dated from 2212 ± 6 Ma to around 2100 Ma; the oldest age, obtained by Pb-Pb evaporation on zircon, has been found on the Niani volcanic suite which has been identified and characterized in Guinea by [8], and recognized in Mali by [68]. It is composed of porphyry lavas and pyroclastic rocks (bedded tuffs, pyroclastic breccias) of andesitic to rhyodacitic composition. Its occurrence is the earliest volcanic event identified to date in Guinea and Mali.
The geology of the FGD is still unclear, the facies are hided under a very dense lateritic cover, about 40 to 90 m which prevents any surface geological work; access to the unaltered rocks is only possible by boreholes. The map of the mine, according to [67] [68], shows the predominance of the flyschoid deposits of the metavolcano-sedimentary formations ( Figure 3). As stated by [70], the FGD is hosted by an acid volcano-sedimentary series metamorphosed to greenschist facies. The metasedimentary series correspond to the fine and coarse-grained terrigenous sediments (siltstones, mudstones, arenites, quartz-arenites, arkoses and microconglomerates). They are affected by schistosity, generally subparallel to the stratification, oriented N150 to N180 with a steep dip varying from 50˚ to 90˚ towards W or SW. The metasedimentary series is cut by intrusive and vein rocks, inducing contact metamorphism with formation of granofels [70].

Materials and Methods
The petrographic and structural characterizations of the FGD presented many difficulties due in part to the absence of outcrops or their weakness. The deposit is affected by very deep lateralization which only revealed rare exposures of altered terrain. In order to solve these field constraints, the petrographic study was realized mainly but not exclusively on the drill cores where the sampling was done. The structural study was conducted in the two open-pits called Main Zone and Zone 5, and on the drill cores.

Lithologies
The lithologies of the FGD consist of dominant quartzofeldspathic metavolcano-sedimentary rocks intersected by plutonic rocks of intermediate composition. The petrographic study has been carried out on thirteen selected drill cores samples representative of the major rocks of the deposit.

Metavolcano-Sedimentary Rocks
The metavolcano-sedimentary rocks of the FGD represent a very deformed sequence of flysch type. In general, they strike NNW-SSE and dip steeply (50˚ to 90˚) towards SW. The main facies are metagreywackes, metasiltstones, meta-argillites, slates and schists. Samples were taken from the facies that could be studied in the polarized light microscope.  Under the microscope, the rock shows a granoblastic texture (Figure 4 The matrix of the rock is made up of an inequigranular, fine-grained assemblage of minerals, composed predominantly of quartz, with a lower proportion of plagioclases, biotite, actinolite, chlorite, epidote, calcite and opaque minerals. Actinolite is randomly oriented; it is pleochroic in shades of green and developed on the clastic fraction of the rock. The mineral occurs dominantly as aggregates of elongated prismatic crystals, occasionally as hexagonal prisms. Its size varies from micrometric to millimetric (up to 2.3 mm), some crystals show twinning. Biotite is brown, micrometric to millimetric (0.07 to 1.3 m) but generally micrometric. It is sometimes pseudomorphosed by chlorite which can develop from biotite or amphibole.
The other minerals present but in low proportion are: epidote, sericite, calcite, apatite, rutile and opaque minerals.
2) Amphibole-sulphide bearing metagreywackes: Sample 579 E1-a The rock color is grey and fine to medium-grained ( Figure 4(c)). It contains sulphides and carbonates evidenced by their reaction with HCl.
Under the microscope, the rock shows granoblastic texture ( Figure 4(d)), with random orientation of the clastic grains.
The clastic fraction of the rock is fine to medium-grained. It is composed of plagioclases, quartz, and lithic fragments embedded in a poorly sorted and recrystallized matrix. The matrix, very fine-grained consists of quartz, feldspars, calcite, epidote, chlorite and sulphides.
Feldspar is micrometric plagioclases, up to 300 µm. They are cloudy or brownish-coloured, much altered and often recrystallized into fine grains. Quartz is subrounded to subangular, it is micrometric in size, up to 600 µm and contains fluid inclusions. It appears as single crystal or polycrystalline, and both show undulose extinction as a result of strain. The boundaries between polycrystalline quartz are sometimes sutured. The lithic fragments are mainly composed of fragments of shale or slate. The rock contains also a fragment constituted of plagioclases laths set in an altered fine-grained groundmass; it is probably a volcanic rock fragment.
The matrix consists of fine-grained quartz, plagioclases, amphibole, chlorite, sulphides, and calcite. Some grains of plagioclases show polysynthetic twins. Amphibole is pleochroic in the shades of green; it is a micrometric hornblende, up to 450 µm, which developed on the quartz-feldspar grains. It occurs as euhedral to subhedral, sometimes it is replaced by chlorite. Calcite is micrometric and presents variable forms: some individuals have anhedral to subhedral shapes. Sulphides are micrometric up to 360 µm, they occur often as well shaped with square form, they are dominantly pyrite.
3) Amphibole-biotite bearing volcanoclastic metagreywacke: Sample 464 E1-f The rock is light grey in color, medium to coarse-grained and is crossed by carbonate veins (Figure 4 The matrix consists of very fine-grained quartz, feldspar, sericite, carbonate, epidote and opaque sulphide-type minerals.

5) Andalusite hornfels: Sample 464 E2-b
The rock is dark-coloured and made up of very fine unrecognizable grains with the naked eyes or with a magnifying glass ( Figure 5(a)).
Under the microscope, the rock presents a granoblastic texture ( Figure 5  The porphyroblasts of andalusite are altered, many of them occur as euhedral to anhedral and appear in rhombic-shaped to weakly elongated. They are micrometric, (up to 500 µm), and colourless in plane-polarized light; in cross-polarized light, they show a mixture of sericite, chlorite and opaque minerals. Andalusite shows locally numerous dark inclusions arranged in the centre, and propagate towards the diagonals, drawing a typical cruciform pattern of graphite rich inclusions. This type of andalusite is commonly called chiastolite. Open Journal of Geology The quartz is more dominant than the plagioclases in the matrix or groundmass possibly former glass. It is micrometric (up to 250 µm) and appears more or less flattened with undulose extinction, the plagioclases show sometimes twinning.
The clay matrix is composed of very fine-grained components which are indistinct. The dominant very fine-grained matrix contains indistinct quartz and feldspars.

Quartz Veins
Under the microscope, the rock shows a granoblastic texture marked by an association of quartz and plagioclases in a minor poorly sorted matrix of micrometric size (Figure 6  2) Sulphide-bearing chlorite-quartz vein: Sample 468 E5-a It is a filament of milky-white quartz, made up mainly of quartz veinlets, sulphides, chlorites and carbonates, observable with the naked eyes ( Figure 6(c)).
Under the microscope the vein shows a granular texture formed mainly by the spectacular development of sutured crystals of quartz in a matrix composed of quartz, plagioclases, chlorite, calcite, sericite, epidotes and opaque minerals (Figure 6(d)).
The dominant crystals of quartz are millimetric and may exceed 5 mm in length. They are anhedral, sutured and strained. They expose undulose extinction and occasionally some subgrains. The phenocrystals of plagioclases are micrometric, up to 600 µm and subhedral. Calcite has variable shape; it occurs in free form or in an aggregate of grains which cut the crystals of quartz. This shows its late character compared to quartz. The chlorite has a dark blue interference colour in crossed-plane polarized. It is associated with sericite, epidote, sulphides and carbonates.
The rock shows a granular texture under the microscope and displays dominant quartz in a matrix composed of quartz, carbonates, and rare muscovite ( Figure 6(f)).
Quartz is micrometric in size and occurs as anhedral strained crystals which display undulose extinction or subgrains.
The matrix is poorly sorted with dominant micrometric grains of carbonates which intersect or grow between the quartz.
The plagioclases phenocrysts are elongated and heavily altered. They vary in size (approximately 1 to 2.5 mm) and are transformed in a mixture of feldspar, quartz, sericite, chlorite, opaque and epidotes. The feldspars present in the groundmass are micrometric and granular. The quartz occurs in the form of anhedral grains of micrometric size (50 to 450 µm). The amphibole is generally retromorphic, biotite is brown, micrometric in size (200 to 400 µm).
Chlorite occurs in micrometric size (200 to 920 µm) with varying shapes. Some individuals show an elongated subhedral form. Chlorite is weakly pleochroic in the shades of light green. It pseudomorphosed both amphibole and biotite. Calcite is anhedral and granular; its size varies between 60 to140 µm. It intersects the chlorite and therefore appears to postdate it. The accessory minerals are rutile and leucoxene.
2) Microtonalite: Sample 037 E2-a It is a leucocratic rock with a fine-grained structure. It is made up of visible dark chlorite and light feldspars (Figure 7(c)).
Residual plagioclases are completely altered; alteration gives a mixture of chlorite, sericite, epidote. Some phenocrysts show occasionally twining which allow them to be identified.
The matrix of the rock is composed of plagioclase, quartz, chlorite, epidote and opaque minerals. The plagioclases vary in size (50 -300 µm); many of them are euhedral and show a twining, some of them form an association in a cluster that looks like a bouquet of flowers. Chlorite occurs in the form of small aggregate grains of micrometric size (<50 µm). It invades and pseudomorphoses massively a former crystal which could be amphibole. Opaque minerals are abundant and dispersed in the micrometric matrix. The calcite shows poorly crystallized grains but it still identifiable by its high birefringence and by the presence of cleavages on the well-formed sections. Epidote is often seen with chlorite.
The accessory minerals are zircon and leucoxene.

3) Quartz diorite: Sample 466 E2-d
The rock is mesocratic, fine-grained; it is made up of quartz, plagioclases, amphibole and biotite, all visible to the naked eyes (Figure 7(e)).
The rock shows a porphyritic granular texture (Figure 7(f)) with a dominant plagioclases, amphibole and biotite.
The plagioclases are altered and micrometric, up to 900 µm. The alteration obliterates their original form; it gives a mixture of white mica (sericite) and epidote. Very rare phenocrysts show twining. No K-Feldspar has been observed. The amphiboles are micrometric to millimetric (up to 3 mm), prismatic or elongate, free or in aggregate. They are pleochroic from pale to green pale and develop on quartz and plagioclases. Biotite is micrometric to millimetric (up to 1 mm), brown-coloured and occurs as subhedral, it replaces locally amphibole.
The recrystallized matrix of the rock is formed mainly of quartz, plagioclase, biotite, calcite chlorite, epidote, apatite and opaque minerals. Quartz is micrometric; it presents xenomorphic form and shows discrete undulose extinction. Chlorite is also micrometric and has variable forms; it pseudomorphoses both amphibole and biotite.
The accessory minerals are apatite and opaques; apatite in elongated (up to 1.5 mm) or hexagonal sections (up to 230 µm). 4) Quartz diorite: Sample 466 E1-c It is a dark coloured rock, medium-grained with a granular porphyric texture (Figure 7(g)). The facies are cut by carbonate veins and locally contains carbonates in the matrix.  Under the microscope, the rock consists of phenocrysts of plagioclases, amphiboles and biotite dispersed in a recrystallized matrix (Figure 7(h)).
Plagioclases are heavily altered and give a mixture of sericite and epidotes. The weakly damaged crystals show a millimetric size up to 2.3 mm. The older phenocrysts are generally replaced by new grains of plagioclases largely present in the matrix. Amphiboles are micrometric to millimetric (0.6 -3.5 mm), and slightly pleochroic in the brown tones. The phenocrysts are in elongated or hexagonal prismatic form. The elongated crystals could attain 3.5 mm. Both are twinned and pseudomophosed locally by biotite. Quartz is micrometric to mil- The other accessory minerals are apatite, rutile, and opaque minerals. Apatite is the dominant accessory mineral. It is in the form of elongated euhedral prismatic crystals or in a hexagonal section. The elongated crystals are micrometric to millimetric, up to 1.5 mm.

Stratigraphic Column
The laterite forms a width crust which prohibit any observations on the outcrops, the stratigraphic column proposed here have been identified on the basis of the study of a representative hole (KDD16-470) of cores drilling (Figure 8). The hole is deep to 350 m, and dips steeply to the NE (50˚), it is perpendicular to the metavolcano-sedimentary rocks.
The rocks of the FGD are organized from top to bottom towards the protolith into several units: lateritic duricrust, saprolite, saprock and unweathered rocks.
Duricrust occupies the top of the stratigraphic column; it is indurated and enriched with iron. It forms parts of deep-weathering profiles. Its thickness is 3 meters.

Structures
The analysis of the structural data collected in this study allowed us to identify

Ductile Deformation
The rocks of the FGD exhibit steeply dipping foliation, the main marker of this deformation is the foliation-S1. In the open-pits, it developed remarkably in the fine-grained facies on the west side. The foliation-S1 has been identified and measured in the open-pits (N = 195) and on the drill cores (N = 40). In both cases, it is parallel to the stratification-S 0 (Figure 9(a) and Figure 9(b)). This parallelism defines an S 0 -S 1 composite surface which trajectories are fairly homogeneous in the open-pits and on the drill cores. In either case, it strikes between N130˚ and N180˚. Its dip direction fluctuates between SW to W and its values range from 50˚ to 90˚ (Figure 10 and Figure 12)

Ductile-Brittle Deformation
In the FGD, there are two types of bodies of minerals which have been precipitated into the fracture within rocks: 1) en-echelon tension gashes, 2) and a quartz vein arrays. The former marks the ductile-brittle deformation recognized in the deposit.
The tension gashes are organized en-echelon, some of them are curveted (Figure 9(c)). They have been observed locally at the west side of the main open-pit at its level 365 m. They extend to the length of 1.4 m, with an opening of a few cm thick (7 -20 cm). In the open-pits, shear fabrics indicate dextral movement in the NE-SW direction (Figure 9(c)).
The quartz vein arrays have been observed and measured in the open-pits (N = 187) as well on the drill cores (N = 42). They intersect all the lithologies of the deposit and seem to be later. The quartz vein arrays have a millimetric to centimetric thickness and rarely reach the meter. However, locally in the open-pits, some veins show a length varying between 1 and 3 m. In the open-pits two sets of quartz vein arrays are secant on the S 0 -S 1 surface (Figure 9(d) and Figure  9(e)), while one is parallel to it (Figure 9     a second set of population labelled QV 2 : it strikes N40 to N80 (NE-SW to ENE-WSW) and dip more steeply (65˚ -85˚) towards the SE, NW or SSE;  a third set of population designated QV 3 with an E-W trending and a dip varying between 6˚ to 70˚ towards the S or N. Some shifts between the quartz vein arrays have been observed locally in the open-pits, in particular between QV 2 and QV 3 , the latter being shifted in a dextral movement. However, most of veins crosscut each other; they seem to be contemporaneous, even if field observations do not allow an obvious relative chronology to be established between the three sets of populations. The most mineralized veins show an NE-SW trending with a dip toward SE [71].

Brittle Deformation
It is marked by faults and fractures which have only been observed and measured in the open-pits (Figure 9). They display several directions; some of them are sub-parallel to the S 0 -S 1 , others are totally sequent.
Structural analysis of the trending of the faults shows two (2) main directions ( Figure 10):  NNW-SSE trending with a shallow dip to the ENE;  ENE trending with a shallow dip to the SSE.
The NNW-SSE faults correspond to reverse faults while the ENE directions seem to be linked to a shear zone.
The fractures show late characters, they cut the quartz vein arrays. Analysis of the density of the poles of the fractures does not show any preferential orientation on the stereogram, and on the rosette (Figure 10).

Lithostratigraphic and Intrusive Units of the FGD
The FGD lithostratigraphic context is dominated by an alternation of fine to very fine-grained metavolcano-sedimentary rocks with subordinated clastic medium-grained facies; all are of Paleoproterozoic age. They are made of metagreywackes, metasiltstones, meta-argillites, slates and schists. This sequence represents a flysch type unit. The sequence is intersected by small dioritic bodies, as well as tonalitic dykes; granitic and monzonitic rocks (Figure 3) have been reported by [68] but we did not identify them in the open-pits or the drill cores. Despite the fact that there is no geochronological data on the deposit, we can assume that the sedimentation occurred between 2125 Ma and 2092 Ma, if we compared it to what is known in the adjacent and neighbouring areas of Siguiri and Massigui. In the Siguiri basin, sedimentation took place between ca. 2124 ± 7 Ma and 2092 ± 5 Ma [38]; a period similar (ca. 2125 ± 8 Ma -2092 ± 7 Ma) to that of the sedimentation of the Massigui region recognized by [15].
In the sample 579 E1-a, the boundaries between the crystals of polycrystalline quartz are occasionally sutured. This is generally a characteristic of quartz from metamorphic sources. The fragment with plagioclase laths dispersed in a finegrained altered matrix of the same sample is probably a volcanic rock fragment. A volcanic origin has been also found on the sample 468 E4-a whose quartz shows locally straight edges; this quartz seems to develop from well-developed phenocrystal a characteristic of volcanic quartz.
The Sample 468 E4-a contains quartz with locally straight edges; it seems to develop from well-developed phenocrystal; this characteristic suggests that it could have a volcanic origin. This sample contains amphibole too; this mineral is generally part of the paragenesis of metamorphosed sedimentary rocks with basic protoliths. From this observation, we consider that the protolith of the sample 468 E4-a, which is a metagreywacke, would initially be magmatic. For this reason, it has been identified as an amphibole bearing volcanoclastic metagreywacke.
The study of the mineralogical assemblages of the matrix of metavolcano-se- Locally, a fine-grained volcano-sediment is transformed into andalusite granofels (sample 464 E2-b), due to the contact metamorphism generated by the emplacement of an intrusive rocks. However, the sample 037 E1-e identified as an andalusite slate presents a foliation materialized by the stretching of the andalusite porphyroblasts. This andalusite slate could be the product of a regional metamorphism that affected the andalusite granofels. Therefore, the rocks of the deposit show a history inherited from contact metamorphism and regional metamorphism; the contact metamorphism seems to be prior to the regional metamorphism.
The various origins of the sediments highlighted by this work implies the destruction of an ancient, exposed crust in a volcanic environment who contributed to the production of clasts of volcanic origin for the sedimentation which could be contemporaneous with volcanism. Afterwards, these rocks will be deformed and metamorphosed in a local and regional setting. They underwent tectonic tightening that affected the region at the closure of the basin.
The stratigraphic column of the FGD described for the first time in a publication essay shows the volumetric importance of metasiltstones and meta-argillites.
These rocks could be related to a volcanoclastic origin since the fine-grained volcanoclastic rocks commonly altered into clay are often classified as shales [72]. Balato of the Siguiri basin described by [38]. According to these authors the formation is dominated by dark grey to light grey massive siltstones beds grading upwards to shales, alternating with cm-thick shale-siltstones and rare fine greywackes interbeds. Across the WAC, isoclinal folding has been described. In the near ca. 2125 -2090 Ma Bagoé basin, composite surface S 0 -S 1 has been reported by [15]. According to these authors, it presents similar strike (NNW-SSE) but dips steeply towards the ENE at the Bagoé Bridge, outside the village of Niamala and in the Banifing River. In the adjacent ca. 2115 -2090 Ma Siguiri basin NNW-SSE oriented folds, due to ENE-WSW compression, have been described by [49].

The Ductile-Brittle Deformation
This stage is poorly expressed in the field. It has been identified through the interpretation of the sigmoidal en-echelon tension gashes filled by quartz. Its extent remains unclear, and there is no evidence of the presence of a large regional The development of the tension gashes is related to the stress field underwent by the rocks when they were buried. It is well known that sigmoidal gashes are related to shear zones which develop at an acute angle (45˚) to the direction of maximum compressive stress given by the tip of the gashes. In the deposit, the curvature of the sigmoidal gashes indicates a dextral movement in the NNE-SSW direction which results from an ENE-WSW regional shortening.
In the Kalana deposit, a set of sinistral sigmoid tension gashes related to an ENE-WSW compressive stress has been identified by [76]. The opposition between the kinematics of shearing at Faboula and Kalana suggests that these two deposits are located on opposite limbs of the same fold as evidenced by the similar strike of S 0 -S 1 and its opposite dip direction.
At the scale of southern Mali and the Leo-Man Shield, shearing has also been described from neighbouring NNE-SSW Siekorolé dextral shear zones [77] and the NE-SW to NNE-SSW Banifing sinistral Shear Zone in the Bagoé basin [3] [15] [62] [74] [75]. In the bordering Siguiri basin, at its southern edge not too far from the FGD ductile deformation along sinistral faults occurred after the crystallization of the granodiorites, around 2.08 Ga [8]. These authors related it to a Late Eburnean ENE-WSW shortening. Further in the south, sinistral shearing has also been reported for the Sassandra Shear Zone at the border of the Archean of Kénéma-Man and the Birimian of Baoulé-Mossi domain [55].
Numerous quartz vein arrays show three different orientations within the FGD.
One type (NW-SE to N-S) is parallel to the regional composite surface S 0 -S 1 , while two others (NE-SW to ENE-WSW and E-W) crosscut it. Quartz veins arrays have been reported in the Kalana gold deposit; they are controlled by the intrusive granitic rocks [78].
According to [73], there are two groups of quartz veins crosscutting a bedding-parallel schistosity surface, striking N170 and dipping steeply towards the E: 1) a first set of groups which show more irregular measured strikes, roughly N-S but some of them are oriented NE-SW and others E-W; 2) a second set of groups, more homogeneous than the other, with closely spaced veinlets striking NE-SW. Both are coeval according to the authors, a point of view shared by Kusters [76] and [78]. The latter suggested that there are many parallel veins, stacked on top of each other, due to their different strikes and dips, some of them must cross and cut each other.
According to [70], the gold mineralization of the Faboula deposit occurs in the form of free gold and is associated with NE-SW quartz veins steeply dipping to SE, which in this study corresponds to the second set of population labelled QV 2 . A major phase of mineralization commonly associated with quartz veining during a D 3 deformation linked to WSW-ENE shortening and formation of the dextral Siekorole shear zone is described by [77]. In the neighbouring Siguiri basin, gold mineralization is associated with one main and, at least, three minor sets of auriferous quartz veins; the main quartz-vein set shows remarkably con-  [49].

The Stage of Brittle Deformation
The brittle deformation is linked to the late emplacement of faults and fractures.
Fractures are present in number in the area, their measure show that they are randomly oriented. They disrupt the main S 0 -S 1 and the quartz vein arrays and are clearly post faulting. Faults are more regularly oriented than the fractures.
They show orientation similar to the most important attitudes seen in the quartz veins arrays: NNW-SSE and ENE-WSW. The NNW-SSE faults correspond to reverse faults while the ENE directions seem to be linked to a shear zone. They could mark the continuation of the brittle-deformation or they might be a result of a concomitant event developed during a compressive event.

Global Tectonic Context of Folding and Shearing
In the Faboula gold deposit, there is an association of ductile, brittle-ductile and brittle deformations. The essential question is whether these deformations belong to different phases or are they the result of a progressive deformation starting with the ductile type and ending with the brittle type?
The sequence of deformations recognized in the deposit shows a ductile deformation marked by isoclinal folding developed during an ENE-WSW compression event which is also at the origin of a brittle-ductile deformation whose sigmoidal en-echelon tension gashes indicate a dextral movement in the NNE-SSW direction. Thus, the folding and the shearing are related to the same greatest compressive stress σ1. The brittle ductile-deformation is localized in the limb, its whole data set (tension gashes, reverse faults, strike slip faults) is consistent with Riedel's shear structures developed in a compressive regime; the orientations of the faults are in accordance with the R and R' structures.
This type of deformation with folding and shearing, related to the same ENE-WSW compressive stress, could occur simultaneously during a transpressive mechanism. Our interpretation is supported by the fact that the reverse faults strike perpendicular to the main compressive stress σ1 in the same direction as the folds and foliation. Indeed, transpression is a combination of strike-slip faulting, thrust-reverse faulting, and folding [80]. It is the spectrum of combinations of strike-slip and coaxial strain involving shortening perpendicular to the zone [81]. Transpression is commonly associated with oblique plate convergence.
Due to its characteristics, and also because it corresponds more to the D 2 or  [49] in the adjacent District of Siguiri.
The transpressive dextral D 2Fb highlighted at Faboula could be equivalent to the regional D 2 or D 3 deformations recognized at the scale of the Leo-Man Shield. It could be correlated with D 3 of [3], D2 of [79], D3 of [77]; D 2S of [49] and D 3 of [15]. All these middle phases of the Eburnean orogeny are bracketed between ca. 2115 -2074 Ma [3] [15]. The deformation of [77] which best matches the D 2FB is D 3 . The latter is linked to ENE-WSW shortening and the genesis of the dextral Siekorole Shear Zone associated with the development of mineralized quartz veins. In the neighbouring Massigui region, dextral D 3 is indicated by the tension gashes [3]. This phase brittle/ductile in character, is highlighted by fracture cleavage, microfaults and vein arrays; its regional fault drag patterns into the Banifing Fault Zone are consistent with a component of dextral displacement [15]. The folding and shearing associated within the D 2Fb are also in agreement with the D 2 of [79] which is the main deformation phase of the Si- The abundance of quartz veins arrays and their relationship with the deformation structures indicates probably that the mineralization is structurally controlled during a hydrothermal event. They could be related to relaxation or orogenic collapse immediately after the D 4 [77], which is a tectonic event linked with to NW-SE shortening and on-going magmatism.

Conclusions
This study gives a new idea of the nature and the spatial organization of the Paleoproterozoic formations of the FGD and the deformations associated with them. Drill cores, for example, revealed geological features of objects that do not appear on the surface. All this testifies to the interest of combining multiple data set in the study of Birimian terrains. The methodology we have adopted is therefore adequate in terms of geological studies for regions with strong weathering and/or strong vegetation cover.
The lithological and structural studies carried out give a general idea of the distribution of rocks and structures in the FGD. All the work, from observation to interpretation, highlights the following conclusions. In the light of the results obtained during this study, the FGD remains interesting for even more in-depth studies in order to update the typology of this deposit compared to others located in the south of Mali and even in WAC.
In terms of perspective, it would be interesting to focus future work on updating the lithological data from the drill cores and the pursuit of structural studies in order to propose a reliable geological model of the subsoil given the significant lateritic cover. This work will naturally have to be done with the interpretation of geophysical data. This will facilitate the understanding of the deposit and will undoubtedly promote its better exploitation.