At the scale of West African Craton, the transition zones between greenstone belts and sedimentary basins can be observed to a large extent in Côte d’Ivoire, Burkina Faso, Niger, western Mali, Guinea, Ghana… and in Senegal.

In Burkina, the western part of the geological formations is in the form of three greenstone belts: Boromo, Hounde and Banfora generally oriented North North-east to North-south ( Castaing et al., 2003 ; Baratoux et al., 2011 ; Metelka et al., 2011 ) associated with basins of late fine-grained sediments of Birimian age.

The transition zone between the Banfora belt and the basin is marked by the Greenville-Ferkessedougou-Bobo Dioulasso dextral shear zone (GFBSZ) intruded by synkinematic granites ( Lemoine, 1988, 1990 ). The Boni shear marks the contact between the Hounde belt and the basin composed of late Tarkwaien’ type sediments ( Baratoux et al., 2011 ; Koffi et al., 2016 ). In the Boromo area, the belt/basin transition is marked by two margins: an eastern margin made up of intermediate volcanics and several ultramafic bodies, and a western margin made up of mafic bodies (basalt, pillow, orthoamphibolite/pyroxenite gabbro). A tectonically controlled basin bounded by the Ouango-Fitini shear zone to the West and the Boni shear zone to the East ( Lüdtke et al., 1999 ).

Ivory coast the Birimian consists of volcano-sedimentary furrows that are generally oriented North-south to North-east (N020 to N050) and intercalated between granitoid batholiths. Several furrows have developed in the Dabakala region: the Haut-N’Zi, the Fettêkro and the Haute Comoe. They are composed of eruptive formations, volcano-sediments and sediments. The western part of the Upper N’zi furrow is mainly covered by metasediments ( Arnould, 1961 ). The Upper Comoe belt is an assemblage of Birimian metasedimentary and metavolcanic rocks. The contacts between volcanic belts and sedimentary basins have not yet been clearly defined, but there are numerous northeast-southwest fault structures in the northeast domain and North-south fault structures in the central part. These are interpreted as the result of two major deformations: the first is the result of tangential tectonics that produced structures oriented North-south to North-North-east, to South South-west ( Feybesse et al., 1989 ); the second corresponds to transcurrent deformation, marked by the emplacement of large granitoid complexes around 2.1 Ga ( Lemoine, 1988 ; Ledru, et al., 1991 in Feybesse & Milesi, 1994 ).

In Ghana, two-thirds of the country’s surface area is dominated by Paleoproterozoic birimian formations composed of NE-trending volcanic belts separated by basins.

In the South-west of Ghana, the Birimian comprises a sequence of volcaniclastics and sediments mainly composed of fine grains and separating a series of four greenstone belts trending North-east to South-west and corresponding from West to East to the Bui, Sefwi, Ashanti and Kibi-Winneba belts. These belts are separated by three Sunyani, Kumasi and Akyem (or Cape Coast Basin) and Agyei Duodu et al., 2009 ). These greenstone belts and sedimentary sedimentary basins were formed and deformed during the Eburnian orogeny ( Bonhomme, 1962 ).

The Sefwi greenstone belt is mainly composed of metamorphosed tholeiitic lavas, some volcaniclastics and synvolcanic tonalitic granitoids with granodioritic granitoids.

The centre of the Sefwi belt is largely granitoid with only minor amounts of Tarkwaian.

The Ashanti greenstone belt is one of the belts. The southern part of this belt is characterised by three volcanic lobes, consisting of basaltic flows, andestic lavas, pyroclastic and sedimentary rocks, with an intermediate granodioritic plutonic suite. Mafic to ultramafic bodies also encroach on part of the volcanic belt. The largest mafic to ultramafic body has recently been interpreted as a paleoproterozoic ophiolite complex in the supra-subduction zone ( Attoh et al., 2006 ).

The Sunyani-Comoe basin is intruded by numerous granitoids ranging in composition from tonalite to peralaminous granite. Zircons studied in the leucogranites immediately adjacent to the Sefwi belt give an age of 2088 ± 1 Ma ( Hirdes et al., 1992 for the Kawtiago granite, Ghana). Published field studies show internal deformation microstructures with a sub-vertical foliation and a sub-horizontal stretching lineation, both parallel to their elongation direction ( Vidal et al., 2009 ).

The Kibi-Winneba volcanic belt is located in the southeastern part of Ghana within West African Craton. It is characterised by volcanic lobes formed of basaltic flows, andestic lavas, pyroclastic and sedimentary rocks, with granitoids occupying intermediate positions.

The Kumasi Group in the Kumasi and Akyem basins formed under an extensional regime during D2 deformation phase (stage 4 of Feybesse et al., 2006 ) where major faults, Ashanti and Akropong, acted as primary basin-forming structures and detachment surfaces prior to D3 reactivation.

At the transition between the basins and the volcanic belts are small outcrops of cherts, carbonates and manganese-rich sediments, which are thought to be the exhalative remains of the eruptions that formed the volcanic belts. This transition zone between the volcanic belts and the sedimentary basins is marked by chemical facies, which have been recognised as the site of much of the gold mineralisation in Ghana.

In Niger, Birimian of Liptako (NE edge of the Man Ridge) are alternating belts of green rocks and granitoid plutons trending North-east ( Dupuis et al., 1991 ). There are three belts: Gorouol belt, Diagorou-Darbani belt and Sirba belt.

The Gorouol belt is made up of metabasites (more or less coarse metabasalts with pillow flow, metagabbros, metadolerites).

The Diagorou-Darbani belt is the central belt of the region. This belt is composed of low-grade metamorphic rocks (tholeiitic metabasalts with pillow structures) and medium-grade metamorphic rocks (garnet-amphibolites, garnet-free amphibolites and micaschists).

The Sirba belt shows metabasites (basalt, dolerite and gabbro), metavolcanoclastites (volcanic rock, tuff and cinerite) associated with metasediments (siltstone, pelite, quartzite, greywacke, chert, conglomerate), and mainly acidic magmatic rocks (granite, granodiorite, diorite, rhyodacite, rhyolite and granophyre). The volcanic and sedimentary formations are generally metamorphosed into greenschist facies and, locally, into epidote amphibolite facies.

The Sirba basin is composed of metasediments (siltstone, pelite, quartzite, greywacke, chert, conglomerate) and magmatic rocks.

The Diagorou-Darbani basin is formed by metasediments, talcschists, chloritoschists and conglomerates.

The deformation undergone by the Neoproterozoic sandstones of the Liptako (Karey Gorou, Niger) on the eastern margin of the West African Paleoproterozoic craton, is essentially materialised by a dense network of faults. Fractures due to a distensive episode, resulting from the reactivation of Mesoproterozoic fractures (around 1400 Ma) during the Pan-African cycle, and fractures linked to three Pan-african compressional phases, represented by episodes with North North-west-South South-east, West North-west to East South-east and West South-west to East North-east directions could be distinguished ( Dercourt et al., 2000 ).

In Mali, four (4) volcanic belts (Yanfolila belt, Morila belt, Syama belt and Faleme belt) are associated with four sedimentary basins (Siguiri basin, Bougouni-Kekoro basin, Bagoe basin and Koffi basin).

The Birimian of South-west Mali is defined by a succession of North-east to South-east oriented units ( Milési et al., 1986, 1992, 2004 ) as a succession of greenstone belts and sedimentary basins.

There are four (4) volcanic belts: the Yanfolila belt, the Morila belt, the Syama belt and the Faleme belt.

The Yanfolila belt is around 60 km wide and contains arc-type volcanic formations, known locally as the “Nani volcanic formation,” and reworked sequences of greywackes similar to those found in the Siguiri basin. The Yanfolila volcanic belt develops along the Yanfolila shear zone is characterised by the emplacement of basaltic rocks to the North of Yanfolila and acid pyroclastics and sediments of a sandstone-pelite nature to the South of Kangaba ( Girard et al., 1998 ).

The Morila belt is around 50 km wide and lies along the vast Bougouni granite domain that occupies the central part of South-west Mali. The Morila Belt also contains basaltic to andesitic lavas interbedded with a suite of volcano-sedimentary formations; felsic intrusions have been dated from 2132-2097 Ma ( McFarlane et al., 2011 ).

The Syama belt is the narrowest, about 30 km wide and lies along the Mali-Burkina Faso border. The Syama belt is broadly similar to the Yanfolila belt but is structurally much more deformed with overturned series. These different formations are intersected by plutons (Finkolo diorite dated at 2049 ± 38 Ma, ( Liegeois et al., 1991 ) and massifs granitoids.

The Faleme volcanic belt is formed from West to East by the Saboussire formation and the Keniebandi formation.

The Saboussire formation a combination of volcanic and volcano-sedimentary facies. This formation occupies the North-western half of the window (from Kedougou to Kenieba). In the southern part, it forms a band of several kilometres wide along the Faleme river. Throughout the formation, there is a clear predominance of volcanics, which decreases towards the eastern edge where sediments dominate Bassot (1966) .

Three major shear zones have been noted in the Mali sector: Banifing, Sassandra and Siekerole. The Siekerole shear is located between the Yanfolila belt and the Siguiri basin. The Banifing shear located between the Morila volcanic belt and the Bougouni basin extends to the South through the Sassandra fault.

The North-est to South-west trending Faleme volcanic belt, intersected to the East by the regionally significant Senegalo-Malian fault, forms the boundary of a narrow post-Eburnian graben. There appears to have been significant displacement along the fault or one of its parallel aftershocks, as the terrain to the East of the Senegal-Malian shear consists of birimian basin sediments (known as Kofi series in Mali).

The lithostructural and geochronological work carried out in the Baoule Mossi domain and in the Kedougou-Kenieba inlier supports a polycyclic evolution of the Eburnian orogeny ( Bard, 1974 ; Milési et al., 1986 ; Ledru et al., 1988 ; Bertrand et al., 1989 ; Feybesse et al., 1989 ; Boher et al., 1992 ).

In Guinea, the belts are formed by:

-a high-quality gneissic complex ( Roques (1948) and here called Guinean Gneiss), including banded and local migmatic orthogneiss, paragneiss, micaschist, base rocks (amphibolite, amphibolo-pyroxenite and pyroxene - garnet metabasite), quartzite, iron quartzite (with pyroxene and garnet) and sparse ultrabasite;

-a plutonic suite, composed mainly of tonalite, granodiorite and granite, which transforms into two major batholiths, the Macenta to the West and the Tounkarata to the East.

-volcanic-sedimentary successions, including metabasite iron formations, bands (BIF) and pelitic sediments, which form elongated narrow belts (Nimba and Simandou belts) discordant with the Guinean Gneiss ( Roques, 1948 ); and

-small leucocratic biotite and granite plutons intersecting the Guinean Gneiss.

The Nimba Mountains series outcrops at the heart of a vast asymmetrical synclinorium oriented North-east to South-east. The North-western flank of this fold is locally very upright and inverted. The South-east flank dips at 30˚C - 60˚C and gives access to most of the lithotectonic pile composed of three (3) similar formations, separated by internal syn-Dl thrust planes, which are responsible for the doubling of the lithological stack. Most complete formation comprises, from bottom to top:

-grey and black silts, shales with intraformational conglomerates passing laterally and/or upwards pure quartzites of conglombratic levels; The facies contain lenticular intercalations of metabasites and carbonate intercalations (Ca or Mn);

-ribbon quartzites and ferruginous (BIF).

The Simandou series also outcrops at the heart of a north-south trending synclinorium ( Feybesse & Milési, 1994 ). The same lithologies are found but in variable proportions: the silt-shale-pure quartzite-amphibolite association may be absent or reduced to one of the last two components (by stratigraphic and/or tectonic bevelling I). Finally, there is a possible transition from the volcano-sedimentary unit to carbonate arkosic sandstones. Here too, reconstructions of the lithotectonic pile reveal tectonic redoubling.

In Senegal, Bassot (1966, 1987) subdivided the western part of the Kedougou-Kenieba inlier into two supergroups arranged in elongated NNE-SSW bands: Mako and Diale-Dalema.

In 2002, in the eastern part of the Kedougou-Kenieba inlier, Hirdes and Davis completed the structuring of the Senegal side by highlighting the Faleme volcanic belt ( Figure 1 ).

The Mako/Diale transition zone is represented by the interface between the Mako volcanic belt and the Diale basin. It is made up of greenstone from the Mako belt, mainly basic volcanics, intermediate to felsic volcanics composed of andesitic lavas and abundant volcanoclastites interbedded with metasediments and metavolcanosediments. Concordant and discordant plutonic masses are also found. This study focuses on the transition zone between belts and Diale paleoproterozoic basin in Senegal.

The stratigraphy of the Birimian formations has long been debated in the West African Craton (discussed in Vidal et al., 1996, 2009 ; Baratoux et al., 2011 ; Kock et al., 2011 , Lambert-Smith et al., 2016 ) and seems to find consensus with Bassot. However, little is known about the transition zones between birimian belts and their associated basins.

Petrographic and structural informations needed to understand their lithostructural architectures is insufficient or non-existent or when it does exist it is not in phase with the new field data. The need to update this information justifies the timeliness of this study in this area.

It is important to note that, despite the paucity of scientific documentation in certain regions, the transition zones between belts and basins in the West African craton remain terrains recognised for their geological potential for the genesis and development of mineralization. These include the Bissa, Inata, Essakane and Mana deposits in Burkina Faso; the Loulo, Kodieran and Gounkoto deposits in Mali; the Bonikro, Agbaou and Tongon deposits in Côte d’Ivoire; and the Sabodala, Massawa, Sofia, Makabingui and Petowal deposits in Senegal.

Major pioneering work done on Kedougou-kenieba Inlier was carried out as part of useful substances prospecting missions by the Mines Directorate of French West Africa: United Nations Development Program (UNDP) in eastern Senegal ( Tagini, 1959 ; Gravesteijn, 1962 ; Bassot, 1963 ).

Petrographic and structural work includes large number of drilled cores giving a fairly accurate idea of the geology of Paleoproterozoic terrains of Kedougou inlier, which locally are heavily lateritic or depositional covered. A lithostratigraphic scale was proposed by Mission Sénégalo-Soviétique de recherches minières (1972-1973) and Bassot (1963, 1966) .

Since Bassot (1963, 1966) , the formations of Kedougou-Kenieba inlier have been the subject of numerous studies (see exhaustive bibliography in Pawlig et al., 2006 ; Debat et al., 1984 ; Ngom, 1985 ; Diallo, 1994 ; Ngom et al., 2007 ; Cissokho, 2010 ; Theveniaut et al., 2010 ; Gueye et al., 2007, 2008 ; Lawrence et al., 2013 ; Bassot 1987 ; Dioh et al., 2009 ; Gozo et al., 2015 ; Dabo et al., 2017 ; Labou, 2019 ; Labou et al., 2020 ) and all of which defining that Paleoproterozoic terrains of Kedougou Inlier are represented by the Mako volcanoplutonic belt and Diale-Dalema basin intersected by different generations of granitoids ( Bassot, 1966 ; Mission Sénégalo-Soviétique de recherches minières, 1970-1973 ; Debat et al., 1982 ; Debat et al., 1984 ; Ngom, 1985, 1995 ; Ndiaye, 1986, 1994 ; Dia, 1988 ; Dia et al., 1997 ; Diallo, 1983, 1994 ; Dioh, 1995 ; Dioh et al., 2006 ; Pawlig et al., 2006 ; Gueye et al., 2008 ; Hirdes & Davis, 2002 ; Delor et al., 2010 ).

Bassot (1966, 1987) was the first to draw up a geological diagram of Kedougou-Kenieba inlier based on lithological and structural characteristics. In 1987, he subdivided this inlier into two supergroups arranged in elongated North North-east bands: Mako and Diale-Dalema. The western zone (Mako series) is oriented North North-east for 70˚ North-west ( Debat et al., 1984 ; Ngom, 1995 ) and is intersected by the Badon batholith. Radiochronological data show that the Diale formations (sediments 2096 ± 8 to 2156 ± 10 ( Milési et al., 1986 ); grauwackes 2165 ± 0.9 ( Hirdes & Davies, 2002 ), are younger and based on the Mako volcanic formations (basalt ages between 2063 ± 41 and 2197 ± 13 Ma ( ABouchami et al. 1990 ; Dia, 1988 ); andesite 2160 ± 16 Ma ( Boher, 1992 ); rhyolite 2067 ± 12 Ma ( Gueye et al., 2007 ) a. More recent radiochronological data show the presence of metamorphic and magmatic rocks from the Mako belt dated between 2200 and 2070 Ma ( Gueye et al., 2008 ; Hirdes & Davis, 2002 ; Dia et al., 1997 ; Lambert-Smith et al., 2016 ). Mako belt is the main source of detritus in the Diale-Dalema series. The dominant ages in the Diale-Dalema series range from 2200 to 2100 Ma ( Kone 2020 ).

After Bassot, a lithostructural subdivision of Kedougou Kenieba Inlier with four series was proposed by Gueye et al. (2007) b, Lambert-Smith et al. (2016) on basis of Bassot (1966) and Ledru et al. (1991) . The boundary between Mako and Diale is defined by Ledru et al. (1988 ) at the Main Transcurrent Shear Zone (MTZ) while presence of detritical facies to the western side of this Ledu et al. (1989) boundary raises many questions about extension of sedimentary basin.

Later, Sow (2004) shows that the tectonic evolution of the Mako belt is characterised by three major shear zones such as the MTZ, the Yaakar Transcurrent Zone (YTZ) and the Sabodala Shear Zone (SSZ). The YTZ is a major structure defined at the contact between volcanic, volcano-sedimentary and sedimentary formations. Regionally, this structure appears to define a corridor of deformation with the MTZ where a mylonitic foliation is evident. The tectonites observed are strongly deformed in some places, and some show a line of stretching when plunging to the South or South South-east. This highlights a minor downthrusting of sedimentary units onto volcanic and pyroclastic units across the steeply dipping YTZ.

Diene et al. (2012) define that the MTZ is discontinuous and associated to western and eastern branches with ponytail branches to the South.

Ganne et al. (2012) show that subduction lead to the burial of sediments at around 33 km during D1 compressive tectonic phase. This rock burial stage is followed by decompression of the associated units with a gradual increase in the thermal gradient from 15˚C per Kilometer to around 50˚C per kilometer during the second stage of transcurrent deformation (D2). This second phase is responsible for the amphibolite facies metamorphism at the contact with granitoid intrusions expressed by garnet, staurotide, chlorite, cordierite, plagioclase, kyanite, sillimanite, biotite, ilmenite, rutile and quartz assemblages.

The structural evolution of the Eburnian phase has been interpreted by various authors as being monocyclic ( Leube et al., 1990 ; Abouchami et al., 1990 ) or polycyclic ( Feybesse et al., 1989 ; Ledru et al., 1991 ; Milesi et al., 1992 ; Ledru et al., 1988 , 1991 ) provide the following information: D1 is tangential and responsible for overlapping structures. It is dated at 2100 Ma ( Ledru et al., 1988 ) and has been defined as an overlap ( Feybesse et al., 1989 ; Ledru et al., 1988 , 1991 ; Milesi et al., 1992 ) or a periplutonic deformation ( Pons et al., 1995 ; Vidal et al., 1996 ; Debat et al., 2003 ; Pitra et al., 2010 ; Delor et al., 2010 ); D2 is transcurrent and associated with sinistral submeridian shears. It constitutes a transcurrent to transpressive deformation corridor responsible for Eburnian tectonics marked by major North-south to North-east structures and plutonic intrusions in Proterozoic terrains ( Ledru et al., 1988 , 1991 ; Liégeois et al., 1991 ; Pons et al., 1995 ); D2 is a sinistral transpression with North North-east to South South-west shortening ( Dabo et al., 2018 ). The D3 phase is marked by dextral detachments ( Feybesse et al., 1989 ).

Within the Kedougou inlier, a close spatial association between shear zones and Eburnian granitoids has been established ( Gueye et al., 2008 ), showing a genetic link between magmatism and deformation (shear zones). Phase D1 is linked to crustal thickening ( Gueye & Ngom, 2020 ). Whereas D2 tectonics leads to the folding of the first schistosity in the sedimentary ensemble of the Mako belt in the form of a vast North-east to South-west trending antiform, with an S2 schistosity as the axial plan ( Dabo et al., 2017 ).

Geochemical studies of ultramafic rocks of Mako belt shows for most of auteurs of Mako ( Baratoux et al., 2011 , Dia, 1988 ; Abouchami et al., 1990 ; Diallo, 1994 ; Dioh, 1995 ; Ngom, 1995 ; Diallo, 2001 ; Pawlig et al., 2006 ; Ngom et al., 2007 ; Ngom et al., 1998, 2010 ; Dabo et al., 2017 ; Ngom, 1995 ; Cissokho, 2010 ; of Ghana ( Loh & Hirdes, 1999 ; Attoh et al., 2006 ; Dampare et al., 2019 ), of Katiola-Marabadiassa en Côte d’Ivoire ( Pouclet et al., 2006 ), of Bouroum Yalogo au Burkina Faso ( Ouedraogo, 1985 ) and of Kadiolo au Mali ( Sangare, 2008 ) that ultrabasites correspond to a single entity associated with undifferentiated tholeiitic series. Only the Loraboué ultrabasites ( Beziat et al., 2000 ) are associated with calc-alkaline series described in the West African Craton.

For mafic rocks, some authors show the existence of two types of tholeiites ( Zonou, 1987 ; Baratoux et al., 2011 in Burkina Faso; Ama Salah et al., 1996 in Niger and Pouclet et al., 1996 in Côte d’Ivoire) without specifying the geodynamic context, while others recognise only one type of tholeiite, either tholeiite1 or tholeiite2 ( Dia, 1988 ; Abouchami et al., 1990 ; Diallo, 1994 ; Dioh, 1995 ; Ngom, 1995 ; Diallo, 2001 ; Pawlig et al., 2006 ; Ngom et al., 2007, 2010 in Mako; Sangaré, 2008 in Mali; Loh & Hirdes, 1999 ; Attoh et al., 2006 ; Dampare et al., 2008, 2009, 2019 in Ghana).

Labou et al., 2020 have recently identified three magmatic suites in the Mako belt from three different sources in both mafic and ultramafic rocks. In ultramafic rocks, the three types of association recognised are related to tholeiites 1, tholeiites 2 and calc-alkaline rocks.

Geodynamic context of Mako calc-alkaline series is a volcanic arc ( Bassot 1987 ; Dia, 1988 ; Boher et al., 1992 ; Diallo, 1994 ; Dioh, 1995 ; Moussolo, 2000 ; Diallo, 2001 ; Dioh et al., 2006 ; Theveniaut et al., 2010 ; Gozo et al., 2015 ; Gozo et al., 2015 ).

The geodynamic context of the tholeiitic series is the subject of controversy. Indeed, Bassot (1966) shows that the Mako Group formations were emplaced in an ocean floor environment;

Abouchami et al. (1990) maintain that Mako volcanism was emplaced in an environment comparable to oceanic shelf basalts without the influence of continental crust;

Ngom (1995) , Ngom et al. (2007, 2010) , Cissokho (2010) and Thievenaut et al. (2010) believe that Mako volcanism is comparable to N-MORBs or oceanic shelf basalts;

Dia (1988) and Dia et al. (1997) show that in the northern part of Mako, the tholeiitic volcanism has transitional geochemical characteristics between the N-MORBs and those of the IATs; this brings them closer to tholeiites of immature intra-oceanic arcs or presence of back-arc basalts;

Diallo (1994) , Dioh (1995) and Diallo (2001) maintain that Mako tholeiitic series was placed in an oceanic island arc environment;

Pawlig et al. (2006) define that the rocks of the Mako Group are juvenile and derived from a depleted mantle source in an island arc environment;

Dabo et al. (2017) believe that the Mako mafic-ultramafic complex represents the lower unit of an ophiolite-like lithospheric fragment of the Birimian crust close to OIBs (Ocean island basaltes) or N-MORBs.

Recently, Labou et al. (2020) highlights two tholeiitic series from a separate source and argued that the tholeiitic1 series shows signatures comparable to MORBs, while the tholeiitic2 series and calc-alkaline series are compatibles with an arc environment.

Over entire study area, the practice consisted in carrying out a general survey of the outcrop (power, lifting the extension contour and noting the coordinates given by the Global Position System (GPS). Outcrops were identified, described, and represented on the field minute. Structural data were recorded from measurements taken throughout the field campaigns. The measurements taken are mainly foliation directions and dips, schistosity planes, lineations, fold axes and, for brittle deformations, some fracture planes. The structural data were modelled using Stereonet. The interpreted structural maps were then digitized and processed with Arcview, Micromine and Géosoft. Geological mapping was used to produce interpreted lithological and structural maps. The lithostructural data were used to analyze tectonic structures.

Aeromagnetic surveys involve measuring the Earth’s magnetic field in order to detect local variations due to magnetism. These anomalies reveal the geological structures of the Earth’s crust, particularly the spatial geometry of rocks and the presence of lineaments interpreted as geological discontinuities (faults). Minerals such as magnetite (Fe₃O₄), ilmenite and pyrrhotite are generally present in endogenous rocks, particularly basic to ultrabasic rocks. They are considered ferromagnetic and are responsible for the magnetic susceptibility of rocks, which can be surveyed on the ground or remotely using a magnetometer ( Figure 2 ).

Spectral radiometry or gamma spectrometry is another method of airborne prospecting. It is about recording the gamma radiation emanating from the first few centimeters of the ground. The radiometry is not the propose of this study, it is integrated and combinated to fact-mapped data to redéfine geometric and geological characteristics of large plutonic masses. It highlights the ground levels of 3 elements: potassium (K), thorium (Th) and uranium ( Figure 3 ). Each of these elements characterises a specific type of facies; for example, potassium abundance indicates the presence of an acidic facies such as granite.

Geochemical analyses were carried out using X-ray fluorescence spectrometry or XRF at the University of Lausanne. Twenty-four (24) samples were analyzed, providing in-depth scientific data on the study area. The samples included 2 gabbros, 2 diorites, 3 basalts, 5 andesitic facies, 3 volcanoclastites, 3 granodiorites, 2 granites, 2 volcanosediments and 2 sediments. Five (5) samples belong to diamond drilling holes, the nineteen (19) other samples from field outcrops.

Major element contents of the total rock (SiO₂, TiO₂, Al₂O₃, Fe₂O₃, MnO, MgO, CaO, Na₂O, K₂O, Cr₂O₃ and NiO) were determined on fused disks prepared from 1.2 g of calcined sample powder mixed with lithium-tetraborate (1:5 mixture). XRF calibrations are based on 21 international reference of silica rock. Data are reported on loss of ignition (LI) basis ( Table 2 ).

Trace element analyses (Sc, V, Cr, Mn, Co, Ni, Cu, Zn, Ga, Ge, As, Se, Br, Rb, Sr, Y, Zr, Nb, Mo, Ag, Cd, Sn, Sb, Te, I, Cs, Ba, La, Ce, Nd, Sm, Yb, Hf, Ta, W, Hg, Tl, Pb, Bi, Th, U) were carried out on disks obtained by pressing 12 g of sample powder onto a Hoechst-wax-C support. Trace element calibrations are based on synthetic standards and international silicate rock reference materials. Detection limits depend on the element concerned, but are in the order of 1 to 7 ppm for trace elements and 20 to 80 ppm for major elements. Geochemical data were processed using GeoChemical Data ToolKIT.

Quantitative Evaluation of Minerals by Scanning electron microscope (QUEMSCAN) were carried out at the Mineral resources and geofluids laboratory of the Department of Earth and Environmental Sciences at the University of Geneva. Thin and polished sections made in Ivory Coast at Felix Houphouet Boigny University were used as base samples. QUEMSCAN analysis is mineralogical and petrographic data acquisition system developed by the FEI company (a subsidiary of Thermo Fisher Scientific).

The lithostructural architecture established on the basis of new geological data ( Figures 2-4 ) highlights three major structures: Western shear-contact (CiscoW), Median shear-contact (CiscoM) and the Eastern shear-contact (CiscoE). The CiscoW, CiscoM and CiscoE delineate three major lithostructural domains corresponding to Maco domain, Sesam domain and Diabba domain ( Figure 5 ).

The Western shear-contact (CiscoW) is a North-south to North-east shear located between pillow lavas and andesitic to metavolcanic facies in the western part of area of study ( Figure 5 ). The CiscoW forms the boundary between the Maco and Sesam domains. It corresponds to Sabodala Sinistral Mylonitic Shear Zone (SSZ).

The Median shear-contact (CiscoM) set as sinistral shear made up of two ranges of structures. A main branch that marks the lithostructural contact between Diabba and Sesam domains followed by second order structures. Main CiscoM sets with two branches: the northern branch located to the North of the area of study is oriented North-south. The main CiscoM southern branch is located to the South of the area of study and oriented North-east.

Eastern shear-contact (CiscoE) is a NE-trending dextral strike-slip, mainly regional in extent. It forms the eastern boundary of the Diabba volcanic formation located to the eastern part of the study area. The CiscoE correspond to Main Transcurent shear zone (MTZ).

Maco lithostructural domain is located to the West of the Sesam domain. It is bounded to the West by the Mauritanides and to the East by the CiscoW. Lithologies are represented by metabasalts, ultrabasic, basic, intermediate and acid plutons.

Sesam lithostructural domain is located to the West of the CiscoM and Diabba domain. It is characterised by the presence of a volcanics associated with metavolcanodetritic sequences. Volcanics forms andesitic rock flows alternating with metamorphosed volcanosediments facies.

Diabba lithostructural domain located to the East of CiscoM. It is essentially made up of slightly metamorphosed sedimentary unit associated with volcanic belt. Volcanic belt is formed by a band of volcanoclastites and andesitic sequences that can be observed locally to the north, south and centre of the Diabba domain. Domains are intersected by plutonic complex.

¹HIGH IMPORTANT MESSAGE: Carefully and close look at Figure 5

Maco is not a locality. Maco is not Mako, which means the volcanic belt (including Diale basin) within Kedougou Inlier

Maco represents the upper and western part of Mako bounded to the East by the CiscoW shear zone which is the equivalent of the Sabodala shear zone (SSZ).

Maco, Sesam and Diabba are not representing localities. They stand as names of three lithostructural domains that form, like puzzles of one-piece, the latest lithostructural architecture of the Mako-Diale transition zone. These are new terms introduced by the main author to designate the following acronyms:

MACO: Mako Croute Oceanique = Mako Oceanic Crust;

SESAM: Sequences et Series Andesitiques de Mako = Andesitic Sequences and series of Mako;

The western shear-contact coresponding to Sabodala Shear (SSZ) is North-south to North-east trending fault located between the pillow lavas and the andesitic and metavolcanodetritic facies in the western part of the study area. It forms the limit between Maco and Sesam domains. The CiscoW takes the form of mylonitic shear zone ( Figure 6 , Figure 7 ). In the proximal parts of the CiscoW, the facies are very mylonitised and fine with minerals oriented along the deformation and located on either side of the shear zone. The CiscoW is associated with compressive deformation affecting, in addition to the Koulountou massif, facies representative of the mafic magmatic phase that led to the emplacement of ultrabasic and basic facies affected by folding ( Figure 8 ). The CiscoW shows two directions, North-south branch to the North and North-east branch to the South.

The CiscoM runs sub-parallel to the Western shear-contact (CiscoW = SSZ). The CiscoM ( Figure 9 ) is a ductile then brittle shear zone with a schistosity showing two main directions North-south and North-east with fairly steep dips. It consists of a main structure associated with three other second-order structures. The main structure has two branches: the main branch to the North of the area of study is oriented N010 to N0180 and dips 56˚C to 85˚C. The North-eastern branch is located to the South, trending N044 to N080 and dipping between 63˚C and 90˚C.

The CiscoE corresponds to the Main Transcurent Shear zone (MTZ). It stands as shear-contact that marks the eastern limit of the volcanoclastites associated with Diabba domain. The CiscoE is regional in extent, running North-east to locally North-south. It consists of a main branch that is continuous throughout the area of study and sub-parallel and discontinuous second-order structures. The CiscoE forms the eastern limit of the Diabba volcanic formation located to the east of the study area. It forms a brittle-ductile shear zone with an average thickness of 0.3 meters ( Figure 10 ). Its length covers the entire study area. It marks the eastern contact between the volcanic and sedimentary formations of Diabba in this area of study. CiscoE is marked by a brittle-ductile deformation and intense graphite or else by breccia or regional brittle deformation.

They are mainly represented by massive or pillowed ( Figure 11A , Figure 11B ) metabasalts and ultrabasic, basic, intermediate and acidic plutonic formations such as ultrabasites, gabbros, diorites, granodiorites and granites.

Dacites are greyish-green effusive rocks rich in quartz and plagioclase. They are weakly porphyritic lavas with plagioclase phenocrysts and microphenocrysts. Calcite and quartz veinlets are present ( Figure 11A ).

Sesam is mainly represented by andesitic volcanic formations (breccias, meta-andesite, metavolcanosediments, metatufs) associated with andesitc volcanosediments. A complex of plutonic ultrabasic, basic et acid and mafic to felsic volcanics are associated to Sesam formations. Explosive andesitic volcanism formed by accumulations of projections in massive or porphyritic form, or breccias. Andesitic flows alternate with agglomerates, tuffs and abundant volcanic breccia ( Figure 12 ).

Diabba main lithologies are composed of sedimentary facies (fine-grained sediments, schists, quartz veins, cherts, metapelites, conglomerates, grauwackes ( Figure 13 , Figure 14 ) associated with metabasalts, volcanoclastites, metarhyodacites. Diabba formations are affected by a series of structures marked by large-scale folding associated with ductile and brittle shearing. The ductile structures form major shear zones and local sub-parallel thrusting North-east trending. Brittle structures accompaning folding and shearing are represented by fractures and reverse faults.

Dioudioukounkou is a circumscribed North-south trending massive intrusive of almost oval shape with irregular rims covering an area of about 60 km². The Dioudioukounkou granite is composed of automorphous to subautomorphous plagioclase with saussauritic core. Quartz is moderately abundant in small interstitial patches. Chlorite (3% to 3.6%) and green hornblende (1.3% to 1.7%) are widespread. Dioudioukounkou contains two facies (coarse primary facies and finer secondary facies. The primary facies surround the secondary along a quartz vein. Dioudioukounkou contain two enclaves types: basaltic and andesitic. Basaltic enclaves are content relics of slightly deformed minerals (pyroxenes, plagioclases and amphiboles). Andesitic enclaves show plagioclases that have been badly affected by ductile and then brittle shearing after a phase of ductile deformation (folding).

Tinkoto is a rounded to locally subrounded massif. Tinkoto granite outcrops sets in the form of metric-sized balls. It is found in bed of rivers, valleys and within lateritic armour.The texture is most often grainy with light whitish-pink colour reflecting the presence of alkaline feldspars and quartz. It is an unconformable granite. Outcrops occur in the form of scattered blocks rarely exceeding ten metres in diameter. It has coarse to medium-grained texture with an uneven distribution of K-feldspar phenocrysts. Melanocratic enclaves can also be found in the massif. Tinkoto massif also shows veins complex set in fracture network. The veins strike mainly N055 and N010. Facies could locally be grey isogranular, with automorphic quartz (irregular edge) showing undulatory extinction and greyish patches forming. Subautomorphic plagioclases show polysynthetic macles or clear double macles. Other facies show heterogranular micrograined texture. Clear sections often include green hornblende or biotite. Crystals may show quartz recrystallisation on edges. Plagioclase crystals are automorphous and sometimes grouped in polycrystalline clusters. Biotite occurs as automorphous sheets, locally embedded in plagioclase.

Koulountou pluton ( Figure 15 , Figure 16 ) is an elliptical massif, narrowed and stretched in its northern part in a North-east direction. It takes the form of blocks that can be several metres in diameter. They are mainly located in the South of Sofia deposit and composed of plagioclase, amphibole, and quartz. They are strongly altered in carbonate-quartz, sericite and pyrite. The main types of alteration are chlorite, sericite, carbonate, limonite and leucoxene. The rocks are also crossed by aplites in places. Deformation is visible in minerals and is made up of fractures. The walls of these fractures are lined with chlorite in places. Note that the late veins are more acidic, with pinkish tinge tending towards a granitic composition. The minerals vary in size, becoming larger to the South.They are only slightly deformed and are made up of fractures. The walls of the fractures are lined with chlorite in places. The late veins are more acidic, with pinkish tinge tending towards a granitic composition.

Tiguida pluton ( Figure 17 ) outcrops to the South of the Koulountou massif over several kilometres along strike N032 in an elliptical shape. It is facies rich in potassic feldspar. Mineral composition shows plagioclase-Ab-Ol (54.11%), Quartz (29.49%), Illite (5.60%), Muscovite (4.89%), Calcite (2.24%), Chlorite (1.86%), garnet granite (andradite). It shows large fracture network mainly oriented N050/80 with surface alteration revealing relics of acicular and coarse grains quartz.

The study (majors and traces) of the formations of Maco domain lithostructural ( Table 1 ) highlights two groups of magmatic rocks: calc-alkaline volcanic rock and sub-alkaline to tholeiitic rocks, which are plutonic formations.

Volcanics represented by the calc-alkaline basalts have SIO₂ contents of between 56.96% and 57.07% and rare earth contents of between 50.8 and 81.9 ppm.

Plutonic formatios are represented by calc-alkaline diorites, tholeiitic diorites and tholeiitic gabbros. The gabbros and tholeiitic diorites at Maco are slightly enriched in light rare earths, with a LaN/SmN ratio of between 1.17 and 1.74. The Table 1 summarises the geochemical characteristics of the lithological samples (from Maco) on which the analyses were carried out.

The study (majors and traces) of the formations of Sesam lithostructural domain highlights three groups of magmatic rocks that may be tholeiitic or calc-alkaline ( Table 2 ): these are volcanic formations, plutonic facies and volcanosedimentary facies.

Volcanics are represented by tholeiitic andesitic basalts, tholeiitic andesites and calc-alkaline andesites. The SIO₂ content of tholeiitic andesitic basalts and tholeiitic andesites varies between 54.89% and 55.93%. Rare earth contents 23.2 to 46.3.

Calc-alkaline andesites, on the other hand, have an SiO₂ content of 59.44% and a rare earth content of 32.3. The volcanic rocks of the Sesam domain show a low enrichment of light rare earths with a LaN/SmN ratio equal to 1.16.

The plutonic formations are calc-alkaline and are mainly represented by the metal-bearing granodiorites of Sesam. They are moderately enriched in light rare earths, with a LaN/SmN ratio of between 1.94 and 2.55.

The volcanosedimentary facies of the Sesam domain show tholeiitic variety (ech3) with an alkaline content (Na₂O + K₂O) of 1.05% and a calc-alkaline variety with alkaline content (Na₂O + K₂O) of 4.84%.

The tholeiitic variety shows very low enrichment in light rare earths (LaN/SmN below the detection limit). The calc-alkaline variety shows average enrichment in light rare earths (LaN/SmN) ratio 2.22).

The chemical signature of formations of Diabba lithostructural domain are divided into three (3) tholeiitic and calc-alkaline magmatic groups ( Table 3 ):

Volcanics are represented by tholeiitic basalts, tholeiitic andesitic basalts, calcoalkaline andesites and calcoalkaline dacites. The SIO₂ content of basalts and andesitic basalts varies from 47.63% to 53.06%.

Light rare earth contents are 122.4 for tholeiitic basalts and 34.2 for tholeiitic andesitic basalts. Calc-alkaline andesites and calc-alkaline dacites have SIO₂ contents 55.60 to 60.50. Light rare earth contents range from 60.9 to 62.2 for calc-alkaline andesites and from 39.9 to 108.9 for calc-alkaline dacites.

Volcanics of Diabba are enriched in light rare earths with a LaN/SmN ratio equal to 3 for tholeiitic basalts showing high fractionation rate with a LaN/YbN ratio of 11.7. The LaN/SmN ratio is 2.18 for calc-alkaline andesites and 5.3 for calc-alkaline dacites. Plutonics will be dealt in another sub-chapter.

The metasedimentary facies of Diabba domain show a variety (ech30) with an alkaline content (Na₂O + K₂O) of 1.05% and a variety with an alkaline content (Na₂O + K₂O) of 4.84%. The low alkali enriched variety has a low light rare earth content (∑REE: 17.2) with a LaN/SmN ratio below the detection limit). Whereas the variety most enriched in alkalis is richer in light rare earths (∑REE: 40.9) with a LaN/SmN ratio of 2.22.

Magmatism is marked by volcanic and plutonic episodes recorded in lithostructural domains at Maco, Sesam and Diabba. This magmatic evolution is expressed in several volcanic and plutonic episodes marked by the production of six tholeiitic phases from different sources and three distinct calc-alkaline volcanic phases.

Magmatic episodes show that Maco is mainly characterised by unimodal (calc-alkaline) volcanism: the Maco calc-alkaline1 series with a volcanic arc affinity.

Maco tholeiitic plutonism highlights two tholeiitic series from different sources: the Maco tholeiites1 (fractionated mantle diorite) from a high potassium mafic source (high potassium mafic rock), with a volcanic arc affinity and Maco tholeiites2 (gabbros) from a low-potassium mafic source with a volcanic arc affinity ( Table 4 , Table 5 and Figure 22 ).

Calc-alkaline volcanism of Maco is based on a compressive geodynamic environment of an active margin associated with volcanic arc market by volcanic arc basalts (ech.89, ech.70). The calc-alkaline volcanism of Sesam sets as volcanosediments (ech.15) with island arc lavas affinity (in context of Ocean Ridge and floor and calc-alkaline andesites (ech.21) with island arc lavas affinity in orogenic context. Diabba calc-alkaline volcanism sits on active margin compressive geodynamic environment. It is associated with an island arc marked by calc-alkaline andesite (orogenic) island arc lavas and calc-alkaline dacites island arc lavas (orogenic). Sesam volcanosediments represent andesitic (explosive volcanic) deposited materiel with facies ranging from coarse to fine (ash) lithic elements.

The tholeiitic plutonism of Maco is marked by the presence of tholeiitic gabbros from an intra-continental source (pre-plate collision zone) and tholeiitic diorites from a mantle source (fractionate mantle zone). Maco’s tholeiitic gabbros come from a mafic magmatic source with a low potassium content (Low K mafic rock). In contrast, the tholeiitic diorites of Maco are derived from a “High K mafic rock” mafic magmatic source with a high potassium content ( Figure 20 ): diagram of Laurent et al. (2014) . In summary, the Maco tholeiitic plutonism highlights two tholeiitic series from different sources.

The Maco calc-alkaline plutonism is represented by the Maco diorite (ech.63) associated with a geodynamic environment of volcanic arc granitoids (VAG). There is also the Dioudioukounkou (ech.66) orogenic granite. The Sesam calc-alkaline plutonism is underlain by two geodynamic environments: compressive and a compressive to distensive active margin. It is associated with volcanic arc granitoids and intraplate granitoids (WPG): The volcanic arc granitoids (VAG) are calc-alkaline, in active margin context and orogenic (compressive). They correspond to the Koulountou granodiorites (ech.92) and the Tiguida granite (ech.59); the WPG intraplate granitoids are calc-alkaline, active margin and orogenic (compressive). They are represented by calc-alkaline Koulountou granite (ech97). The calc-alkaline Diabba plutonism is based on compressive active margin geodynamic environment associated with volcanic arc granitoids (by Tinkoto granite (ech.81) and Diabba granodiorite (ech.317).

The magmatism of the Sesam arc is marked by MORBs tholeiites associated with arc tholeiites and calc-alkaline series ( Table 4 , Table 6 , Table 7 and Figure 22 ): tholeiites3 of Sesam (ech.18: andesitic basalt) with MORBs affinity from active margin (Ocean Ridge and floor), tholeiites4 of Sesam (ech.13: andesite) with intracontinental MORBs affinity (Spreading center of island) and tholeiites with insulair arc lavas affinity (ech.3 volcanosediments) and calc-alkaline2 series of Sesam with insulair arc affinity fed by two sources with distinct geotectonic contexts (ech.21: andesite in orogenic context and ech.15: volcnosediment with insular arc affinity in Ocean Ridge and floor context).

Tholeiitic volcanism manifests itself in tectonovolcanic episodes belonging to very distinct geodynamic environments: Intraplate basalts (intraplate lavas) with an affinity for MORBs (ech.375 = Diabba basalt); Andesitic basalts (ech.76 = Diabba andesitic basalt) of active (compressive) margin with MORBs or OIBs affinity; Intracontinental (compressive to distensive) andesites (ech.13 = Sesam andesite) with MorBs intraplate affinity; active margin andesitic basalts (ech.18 = Sesam andesitic basalt) with an affinity for island arc lavas; active margin (compressive) tholeiitic volcanosediments (ech.3=Volcanosediments de Sesam) with affinity for island arc lavas. Sesam volcanosediments represent andesitic (explosive volcanic) deposited materiel with facies ranging from coarse to fine (ash) lithic elements.

The Diabba domain is marked by tholeiitic volcanisms and calc-alkaline volcanisms ( Table 4 , Table 6 , Table 7 and Figure 22 ): Diabba tholeiites5 (basalt) with affinity for intraplate lavas (continental zone); Diabba tholeiites6 (andesitic basalt) with MORBs or OIBs affinity (oceanic islands zone) and Diabba calc-alkaline series3 (andesites) with island arc affinity (orogenic).

Six tholeiitic series are associated with six major calc-alkaline plutonic masses ( Tables 1-3 , Table 6 and Figure 22 ):

1) Dioudioukounkou post-orogenic calc-alkaline granite

2) Koulountou post-collision uplift calc-alkaline granite

3) Tiguida Syn-orogenic calc-alkaline granite

4) Preplate collision calc-alkaline granite at Tinkoto

5) Diabba calc-alkaline granodiorite (preplate collision)

6) Koulountou calc-alkaline granodiorite (fractionate mantle)

These large plutonic masses belong to three (3) differents magmatic sources: Koulountou (ech.97) and Tinkoto granites and Koulountou granodiorite come from high-K mafic sources while Tiguida granite and Diabba granodiorite are issued from low-K mafic rocks. Dioudioukounkou granite belongs to tonalite source.

Tectonism is the set of movements that affect the Earth’s crust and cause the deformation, reorganisation or break-up of rock layers. Orogenic tectonism is when movements occur horizontally giving rise to mountains and areas with folds and faults. The results of the work highlight complexes marked by magmatism and backed by orogenic tectonism. These are known as tectonomagmatic complexes. The tectonomagmatic complexes consist of volcanoplutonic formations with distinct geodynamic environments associated with three (3) majors tectonic boundaries: CiscoW, CiscoM and CiscoE. These tectonomagmatic complex are the Maco oceanic crust, the Sesam arc and the Diale back-arc-basin.

It extends from the pre-plate collision zone to the Maco orogenic zone via the ridge zone and the seafloor. The Maco oceanic crust is bounded to the East by the CiscoW shear-contact zone. It is characterized by the production of orogenic late to post-orogenic mafic magmas, mainly represented by calc-alkaline basalts, tholeiitic gabbros and diorites, calc-alkaline diorites and the Dioudioukounkou granite. Calc-alkaline active margin basalts shows volcanic arc affinity. These formations of Maco oceanic complex are intersected by peraluminous ( Figure 20 ), post-orogenic intraplate granite of Dioudioukounkou. Maco volcanism is calc-alkaline ( Figure 18 ) in a subduction context. It is associated with two tholeiitic series: Maco tholeiites1 and tholeiites2 from distinct mafic sources ( Figure 21 ).

Sesam arc extends from the CiscoW shear-contact zone to the interface between the orogenic domain and that of the oceanic islands adjacent to the spreading oceanic ridge. Sesam volcanic arc is marked by basic to intermediate orogenic, syncollisional to post-collisional uplift volcanism, mainly marked by tholeiitic andesitic basalts, tholeiitic and calc-alkaline andesites and tholeiitic and calc-alkaline volcano sediments. These volcanic and volcanosedimentary formations are intersected by the metaluminous, syn-collisional Tiguida granite and by the two plutonic episodes of the compressive active margin of Koulountou: the first represented by the calc-alkaline granodiorites from “fractionates mantle” zone and the second by the post-collisional, metaluminous ( Figure 20 ) uplift granite of Koulountou. The magmatism of the arc is marked by two tholeiitic series associated with a calcoalkaline series: Sesam tholeiites3 with MORBs affinity, Sesam tholeiites4 with MORBs affinity ( Figure 19 ), Sesam arc tholeiites and Sésam calcoalkaline2 series with island arc affinity.

Diale back-arc basin extends from the arc domain to the continent. It is bounded to the West by the CiscoM shear-contact zone. These tectonovolcanic episodes are intersected by the calc-alkaline, peraluminous Diabba granodiorite and the calc-alkaline, metaluminous Tinkoto granite associated with orogenic island arc lavas. Sediments are associated with the continental domain. Sedimentary facies are essentially anorogenic (cherts) and detrital (fine metasediments) settting on volcanics. Diabba back-arc basin is marked by two distinct tholeiitic series associated with a calc-alkaline series: Diabba tholeiites5 with MORBs intraplate affinity and Diabba tholeiites6 with MORBs or OIBs affinity ( Figure 19 ) and Diabba calc-alkaline series3 with an island arc affinity.

The characterisation of magmatism and orogenic tectonism enable to define the geodynamic evolution of lithostructural domains within Mako-Diale transition zone into tectonomagmatic complexes (Maco Oceanic crust, Sesam Arc and Diale back-arc-basin) associated with three major shears: the Western Shear-Contact Zone (CiscoW corresponding to Sabodala Shear: SSZ), the Middle Shear-Contact Zone (CiscoM) and the Eastern Shear-Contact Zone (CiscoE corresponding to Main Transcurent shear Zone: MTZ).

The discovery of the CiscoM and Diabba raises the question of the lithostructural definition of the major shear zones of Mako. The boundary between Mako and Diale-Dalema supergroups, which had previously been established to the MTZ mapped by Ledru et al., 1988 , was redefined in this study. The new boundary is marked by the median shear-contact CiscoM. The Yaakar Transcurent shear zone, defined by Sow (2004) at the contact of volcanic, volcanosedimentary and sedimentary formations and forming a shear corridor with the MTZ, could have been comparable to the CiscoM, except that the latter (the CiscoM) is formed by a main branch oriented North-south to North-east associated with second-order structures. The MTZ remains the eastern lithostructural limit of the volcaniclastic formation along Massawa deposit located within Diale back-arc-basin. It constitutes a dextral shear zone oriented North-east to locally North-south formed by a continuous main branch (0,3 meter wide) over the entire area of study and by subparallel, discontinuous second-order structures. Taking these characteristics into account, the discontinuous model of MTZ from Diene et al. (2012) showing a western branch and an eastern branch with ponytail branches to the South seems out of step with the evidence continuity of CiscoE along its main branch associated with subparallel second-order structures observed to the East of entire area of study.

Maco volcanism is unimodal (calc-alkaline) and marked by the production of volcanic arc basalts in a subduction context. This result confirms the consensus of several authors ( Bassot, 1987 ; Dia, 1988 ; Boher et al., 1992 ; Sylvester & Attoh, 1992 ; Diallo, 1994 ; Dioh, 1995 ; Ama Salah et al., 1996 ; Béziat et al., 2000 ; Moussolo, 2000 ; Diallo, 2001 ; Lahondere et al., 2002 ; Pawlig et al., 2006 ; Sangare, 2008 ; Dioh et al., 2006 ; Theveniaut et al., 2010 ; Gozo et al., 2015 ) showing geodynamic evolution of the calc-alkaline serie wich is associated with a volcanic arc formed in a context of subduction with the only difference that these authors consider all of Mako as homogeneous framework. On the contrary, this study defines Mako as heterogeneous lithostructural framework formed by three lithostructural domains, including Maco located to the West of CiscoW = Sabodala shear zone. Maco is therefore not Mako.

The context of tholeiites has long been debated, and several reference models have been proposed by authors at the Kedougou Inlier scale within the West African craton. Ngom, 1995 ; Ngom et al., 2007 ; Theveniaut et al., 2010 ; argued in favour of a MORB context at Mako, while Zonou, 1987 proposed an N-MORB context at Bouroum-Nord in Burkina Faso. Dia, 1988 ; Diallo, 2001 ; Pawlig et al., 2006 support the idea of an arc environment at Mako, as do Ama Salah et al. 1996 at Liptako in Niger; Beziat et al. 2000 at Loraboue and Baratoux et al., 2011 at Boromo and Hounde in Burkina Faso; Sangare, 2008 at Kadiolo in Mali and Sylvester and Attoh, 1992 ; Attoh et al., 2006 ; Dampare et al., 2008, 2009, 2019 at Ashanti in Ghana). Dioh (1995) argues in favour of a transition between MORB and arc while Dabo et al., 2017 support a MORB or OIB context for the geodynamic formation of the Mako tholeiites.

More recently, Labou, 2019 ; Labou et al., 2020 highlight a dual tholeiitic series with tholeiites1 and tholeiites2 from different sources corresponding to two different geodynamic contexts. The tholeiitic1 has signatures comparable to MORBs, while the tholeiitic2 and the calc-alkaline are compatible with series emplaced in an arc environment. This result defined by Labou, 2019 ; Labou et al., 2020 , which puts data from Lame, Sofia and Koulountou (located to the South-western continuity of the Sesam domain) into the same analysis grid for basic and ultrabasic rocks, is confirmed by our study. However, this result cannot be extended to all Mako representing the volcanic belt integrating Diale basin (this study shows that lithostructural architecture of Mako is made up of three domains: Maco, Sesam and Diabba). Consequently, the tholeiites with signature comparable to MORBs associated with arc tholeiites and the arc calc-alkaline serie ( Labou, 2019 ; Labou et al., 2020 ) corresponds to a partial signature of one domain of Mako. It could be comparable to the result described by Dioh (1995) in favour of a transition between MORBs and arc.

This result is typical of the only Sesam domain associating tholeiites3 (tholeiites1 and tholeiites2 are already cited in Maco) from Sesam with active margin MORBs affinity (Ocean Ridge and floor), tholeiites4 from Sesam with intracontinental MORBs affinity (Spreading centre of island), island arc tholeiites and the calcoalkaline2 from Sesam with island arc affinity (this study). Sesam calc-alkaline2 series with island arc affinity is comparable to island arc model ( Dia, 1988 ; Pawlig et al, 2006 ) which suggests lithospheric convergence leading to subduction. This island arc context is also comparable to that already described in the Mako Group by Dia (1988) , Diallo (2001) and Pawlig et al. (2006) and in the West Africa Craton, in particular at Liptako in Niger by Ama Salah et al. (1996) ; at Loraboue in Burkina Faso by Beziat et al. (2000) and at Kadiolo in Mali by Sangare (2008) .

The context of tholeiites5 (continental basalts) with intraplate MORBs affinity and tholeiites6 with MORBs or OIBs affinity is comparable to that of Dabo et al. (2017) who support a MORBs or OIBs context for the geodynamic setting of Mako tholeiites. Diabba tholeiites5 and tholeiites6 are associated with the calcoalkaline3 series (andesite and dacite) with island arc affinity (orogenic). The context of continental diabba tholeiites5 with intraplate MORBs affinity (basalts) has been evoked in the Perkoa series in Burkina-Faso. The tholeiitic volcanism associated with the subgrauwacke sediments is interpreted as continental basalts emplaced under platform conditions on a continental basement ( Ratomaharo et al., 1988 ). The production of continental basalts in favour of CiscoM rifting in Diabba domain (as defined in this study) has been described at the scale of the West African Craton. In fact, volcanism with an affinity for continental basalts in the Bouroum path was set up in favour of intracontinental rifting according to Kroner’s model. The generation of the volcanic arc and then the island arc with island arc tholeiites (lATs) at the edge of the continent shows the evolution of the rift into a back-arc-basin. This environment is comparable to that described in the Upper Comoe, where isotopic data from the lATs and MORBs basalts suggest that the rift evolved into back arc basin in association with an island arc environment ( Lemoine, 1988 ).

In summary, magmatic differentiation associated with the end of CiscoW would have led to the production of basic to intermediate terms of the Maco volcanic arc complex. This stage of the volcanic arc was followed by tectonic accretion of the Mako belt during the Eburnian orogeny Kone et al. (2020) . The deformation phase D1 linked to crustal thickening ( Gueye & Ngom, 2020 ), corresponds to the mylonitic contact shear zone CisoW corresponding to the Sabodala ductile transcurrent and sinistral shear zone (SSZ) oriented North-South to North-East and recorded between Koulountou pluton and the basaltic facies. CiscoW corresponds to D1. The D1 phase is dated at 2100 Ma ( Ledru et al., 1988 ) and defined as a thrust ( Feybesse et al., 1989; Ledru et al., 1988 , 1991; Milési et al., 1992 ) or a periplutonic deformation ( Pons et al., 1995; Vidal et al., 1996; Debat et al., 2003; Pitra et al., 2010; Delor et al., 2010 ).

This D1 phase is followed by the CiscoM, which separates Sesam island arc from the continental arc. At the end of the CiscoM, tectonics favoured a distension phase leading to tectonomagmatic complex ( Figure 23 ) evolving toward the initiation of Diabba continental back-arc graben associated with the volcanic arc and epicontinental island arc complexes. Plutonic and volcanic formations in context of volcanic arc must have been locally uplifted and eroded to provide the main sedimentary input to the Diale basin. The Mako belt is the main source of detritus in the Diale-Dalema series. The dominant ages in the Diale-Dalema series range from 2200 to 2100 Ma ( Kone et al., 2020 ). D2 phase is the early Eburnean event which involves a sinistral transpressive deformation ( Dabo et al., 2018 ). The opening of Diale back-arc-basin is linkable to CiscoM corresponding to D2 Phase dated 2096 Ma ( Feybesse et al., 1989 ). D2 is transcurrent and associated with sinistral submeridian shears. It is a transcurrent to transpressive deformation, responsible for Eburnian tectonics marked by major NS to NE structures and plutonic intrusions into Proterozoic terrains ( Ledru et al., 1988 , 1991; Liégeois et al., 1991; Pons et al., 1995 ).

The phase D2 (CiscoM) is followed by CiscoE corresponding to D3. The D3 phase is marked by a series of East-north-east dextral detachments ( Feybesse et al., 1989 ). Its manifestations have been found in Guinea, southern Mali and Côte d’Ivoire (Feybesse et al., 1989 ) and on the borders of Ghana and Côte d’Ivoire ( Ledru et al., 1988 ). It is coaxial and marked by subvertical crenulation schistosity S3 N50˚ to N70˚ and straight P3 folds.

In Mako Supergroup, the late magmatic phase due to tardive deformation occurred between 2100-2070 Ma - Gueye et al. (2008) . Eburnian magmatism ceased in the Mako belt after the Eburnian compressive deformation ( Gueye et al., 2008 ) accompanied by the emplacement of the Tinkoto and Saraya plutons (dated by the U/Pb method on zircon at 2074 ± 9 Ma ( Gueye et al., 2007 ). The late deformation, dated at around 2073 Ma, was defined in Burkina Faso ( Feybesse et al., 1989 ). It marks the end of the Eburnian event. This last magmatic activity was characterised by transcurrent tectonics accompanied by magmatism and the closure of the basin.

The closure of the Diale basin is thought to be associated with Late Deformation phase D4 located beyond the D3 phase (CiscoE = MTZ) and associated with the Late Magmatic Phase. This late magmatic event marked by emission of rhyolites and dacites associated with a highly potassic plutonism (Mineral Plan) and garnet leucogranites represents the end of crustal thickening. In summary, the opening of the Diale back-arc-basin is related to D2 = CiscoM, while its closure could be associated to D4. A compilation of the cartographic and geophysical data available in the Dalema could situate the D4 at the level of the Faleme shear-contact (CiscoF). Diabba was formed from D2 to D4 phases. The initiation of Diale basin is related to CiscoM and its closure set along the Faleme shear-contact (CiscoF) located beyong CiscoE. The tectonic evolution of the Eburnian orogeny within Mako-Diale transition zone highlights from West to East four deformation phases : CiscoW, CiscoM, CiscoE and CiscoF respectively running for D1, D2, D3 and D4. These shears-affected contact zones, sites of intense tectonic processes and geological evolution, are sites of concentration of economic minerals such as gold for Sabadala and Sofia deposits along the CiscoW; for Massawa deposit along the CiscoE. This suggests that CiscoM, CiscoF stand as potential host structures for futures Kedougou inlier deposits.

Diabba is an epicontinental graben that forms the back-arc basin associated with Maco oceanic complex and Sesam island arc. Overall, the geodynamic evolution of the Mako-Diale transition zone located within the Kedougou-Kenieba inlier is linkable to a single magmatic event associated with tectonomagmatic episodes ( Figure 23 ). The transition from Maco to Sesam would have taken place through a process of magmatic differentiation leading to the production of tholeiitic suites and calc-alkaline series.