The calc-alkaline volcanic formations in the western part of the Kedougou-Kenieba inlier crop out in three complexes: the Foulde in the North and the areas of Mako and Baniomba in the South. These complexes which either combine with the tholeiites or cut across the sedimentary formations are composed of thin veins and massive lava flows. They have many petrographic similarities and show chemical characteristics that resemble those of island-arc rocks. At the tectonic level, the D1 deformation phase preceding the formation of the basins and the transpressive tectonics including an oblique convergence may account for the structural evolution of the Mako volcanic belt. Its occurrence in different basins may be evidenced by the composition of some lithophilic components like the Sr, Ba, U, Rb and the composition of clinopyroxenes enriched in TiO 2 , FeO, Na 2 O in the Foulde calc-alkaline volcanic rocks that developed in a sedimentary environment.
The Paleoproterozoic (~2.0 Ga Birimian) of the West African craton is characterized by bimodal magmatism with successive tholeiitic-affinity volcanism and calc-alkaline volcanism (Bassot, [
The calc-alkaline volcanic series have been identified in the entire Man rise (MR) and in the Kedougou-Ke- nieba inlier (KKI). They are well identified in Ghana (Sylvester and Attoh, [
The relations between the calc-alkaline series and their enclosing are varied. There are two types of deposits: 1) dykes or stocks cutting the tholeiitic series (Sylvester and Attoh, [
This paper aims to analyze the petrographic, mineralogical, geochemical (rocks and minerals) characteristics of the calc-alkaline series in the western part of the Kédougou inlier and constrain, through a petrostructural study, the geodynamic context of their formation. To achieve this goal, three areas of the inlier have been considered: 1) the Foulde area where calc-alkaline series are interbedded in sedimentary series (Dioh, [
Based on the available topographical and geological maps, the field works are carried out in several areas of the Mako Group identified by Théveniaut et al. [
In Senegal, the Paleoproterozoic appear in the Kedougou-Kenieba inlier (KKI) which, together with that of Kayes, represents the westernmost part of the West African Craton. The KKI is disconformably covered by the Neoproterozoic and Paleozoic geological formations of the Mali and Segou Madina Kouta series in the South, the Faleme (in the West) and the formations of the Taoudeni Basin in the East and North (Bassot, [
The Paleoproterozoic formations of the KKI are divided into two main lithostratigraphic units (Bassot and Dommanget [
The Mako Group consists of basalts with a wide-range of textures (pillowed or massive lavas). Ngom [
An island arc environnement was also proposed for the Paleoproterozoic volcanic formations of the inlier (Diallo, [
The sedimentary and volcano-sedimentary formations of the Diale-Dalema Group in the East of the KKI are mainly carbonate rocks, shales, pelites, sandstones, arkoses, greywackes, conglomerates and tuffs. They are cutted by an intermediate calc-alkaline volcanism (Bassot, [
All the volcanic, volcano-sedimentary and sedimentary formations are affected by regional greenschist-facies metamorphism and are cut by magmatic units comprising various calc-alkaline plutonic rocks (Bassot, [
In the western part of the KKI, calc-alkaline Paleoproterozoic volcanic rocks appear in the East of the Mako tholeiitic series which consist of a North-south-oriented land strip. In this strip, the calc-alkaline rocks have been studied in two areas that stretch from the North to the South: the Mako area (Diallo, [
In Mako and Baniomba, these rocks show subvertical structures and form veins cutting across the tholeiitic formations and also tectonically interlayerings in the tholeiitic basalts, whereas in the Foulde area, the calc-al- kaline rocks are flow-shaped (from basic to intermediate) interbedded in sediments, and specifically highly differentiated units of these units cut across sediments.
In all three areas, calc-alkaline rocks are affected by greenschist-facies Eburnean metamorphism and sometimes by a hydrothermal alteration that often makes difficult to identify primary minerals. Therefore, the identification of petrographic types will be carried out also through the chemical analyses reported on the TAS diagram (SiO2/Na2O + K2O). This diagram shows that the calc-alkaline rocks indicate a differentiated serie with basalts, andesites, dacites and rhyolites. This serie is well represented in all complexes (Foulde, Mako and Baniomba). In addition, the formations appear less altered in the Mako complex than in other areas.
The studied rocks show the same petrographic characteristics whatever the areas. We shall describe the main following types: basalts, andesites, dacites and rhyolites.
Basalts with greenish colour have a microlitic and porphyritic texture including clinopyroxene phenocrysts (about 0.7 × 1.3 mm) and rarely plagioclase. The clinopyroxenes (about 30% of the rock) range from hedral to subhedral, frequently zoned and sometimes twinned, partially altered and even sometimes completely turned into amphibole. The plagioclase (An70), between 5% and 10% of the rock, with is in some rare cases phenocrysts, essentially consists of microlites. Opaque minerals are either included or not in the different mineral phases. Epidote, chlorite, calcite and quartz compose the secondary paragenesis related to metamorphism. Basalts are less voluminous than other facies.
Andesites are the most common rocks in the volcanic complexes. On outcrops, they form metric-sized bodies affected or not by the deformation.
The rocks are dark-coloured or greenish and have a porphyritic microlitic texture with a primary paragenesis mainly containing phenocrysts of pyroxene and rarely plagioclase.
Pyroxene phenocrysts (about 20% of the rock mass) are either euhedral or subhedral and they exclusively contain clinopyroxenes that can sometimes be altered into actinolite.
Plagioclases (An37-56), in most cases are epidotised and without evidence of twinning due to the high alteration level. Secondary minerals are similar to those found in basalts.
Depending on the relative proportions of the two main mineral components, andesites form two sub-facies. The first one, rich in plagioclase (plagioclasites) is found in the Foulde complex only, and the other sub-facies represented by ferromagnesian andesites appear in every complex.
Dacites: These rocks are light coloured and show macroscopically plagioclase and ferromagnesian minerals phenocrysts of different sizes which are coated in a clear aphyric paste. A microscope examination reveals that the original texture of the rock has completely disappeared. It is replaced by secondary texture of the microgranular porphyry-type. The rock contains completely altered plagioclase (20% - 30%), amphibole (10% - 15%) and ancient ferromagnesian minerals that are difficult to identify. Secondary minerals including epidote, calcite, quartz and chlorite are enclosed in primary mineral sections.
Rhyodacites, which are poorly represented in the outcrops, are found in the Foulde and Baniomba complexes. The rock, whose colour goes from gray to light gray or pinkish gray, forms sills or low-power veins. In Foulde, this rock is affected by a cleavage trending 45˚N with a dip of 65° to the North-West.
The porphyric microlitic rock contains quartz phenocrysts (about 20%) of different sizes that sometimes show corrosion gulfs, altered plagioclase (25% - 30%), biotite (20% - 30%) and a secondary paragenesis mainly composed of quartz crocrystals, epidote, calcite and chlorite.
The Rhyolites found in Foulde and Mako complexes are white-coloured (they are altered in such cases) or reddish. They show microlitic porphyric texture associated with automorphic quartz that sometimes present corroded sections or volcanic glass, plagioclase, sanidine and chloritised biotite. Secondary paragenesis consists of chlorite, epidote, calcite and opaque minerals in amoeboid masses.
Pyroclastic rocks: These rocks are andesitic and include tuffs and sometimes breccias. These variedly coloured rocks contain clast minerals (plagioclase, quartz and amphibole) and/or lithic andesitic elements.
Pyroxene chemical compositions and structural formulas results are available in Gozo’s thesis (in preparation). Clinopyroxenes (Cpx) have been only studied in the calc-alkaline volcanic rocks of the Foulde and Mako Groups. They are found in the basaltic and andesitic formations of all complexes. In some facies of the complexes examined, pyroxenes are completely altered into amphibole (actinolite), epidote and chlorite; in other facies, by contrast, altered and unaltered pyroxenes can coexist.
Clinopyroxenes correspond to augites. However, a small amount of clinopyroxenes seen in Baniomba (5%) and a good number of those in the Mako facies (more than 50%) have a diopsidic composition (
With the increase in SiO2 content, lower levels of FeO, TiO2, and Al2O3 are generally noticed, and to a lesser extent, MnO and Na2O. Meanwhile, MgO and CaO levels are increasing, whereas Cr2O3 shows no correlation.
When comparing Cpx in various complexes, we found out that for SiO2 equivalent contents, the Mako rock Cpx are poorer in FeO, TiO2 and Na2O (
The aboundant content of SiO2 (50% - 55%) of the Cpx examined, which is compatible with a saturation of tetrahedral sites (Si + Al = 2), characterizes the subalkaline rocks clinopyroxenes. This trend is confirmed by their position in the Ti − Ca + Na diagram (
The Cpx compositions in volcanic rocks from Mako and Foulde Groups are discriminating and allow the distinction of rocks from the three complexes with a transition for the Baniomba Cpx whose compositions are between those of Mako and Foulde.
Amphiboles have been studied only in the Foulde and Baniomba rocks. No amphibole was found in the Mako complex rocks. Their chemical composition and structural formulas are available in Gozo’s thesis (in preparation).
Amphiboles in calc-alkaline volcanic formations are of calcic. Their TiO2, Cr2O3, NiO and Na2O contents are less than 1%. In the Foulde basalts and andesites, amphiboles include actinolite and actinolitic hornblende. In the Baniomba complex andesites, amphiboles are composed of actinolite.
In the Foulde and Baniomba complexes, amphiboles are metamorphic and they originate from low-pressure metamorphism. Their crystal-chemical evolution has resulted in a decrease in the filling ratio of site A (Foulde) and in the absence of glaucophanic, edenetic, tschermakitic and richteritic substitutions.
When amphibole exists, it usually comes from the alteration of clinopyroxenes. The existence of primary amphiboles may be suspected in some facies and, should the case arise, the presence of chlorite shows that they
have started to alter.
Despite the small number of studies conducted on the amphiboles of the Baniomba complex, it seems that, like clinopyroxenes, amphiboles originating from their destabilization may be discriminating for the characterization of the different complexes.
Plagioclases are minerals that are found in all the rocks from volcanic complexes. They form, together with clinopyroxenes, the primary paragenesis. Their proportions vary according to facies, but on the whole, they remain in lower ratios than clinopyroxenes, except in plagioclasites where they largely (90%) prevail over other minerals. Plagioclase sections are altered or destabilized as epidote, calcite, sericite; they sometimes contain recrystallizations of quartz microcrystals.
In the andesites of the Foulde complex, we essentially find andesine, labrador, and albite and oligoclase are scarce. The andesites of the Baniomba complex rocks are mainly albite. The alterations that occurred in the plagioclases among which the albitisation (Ab 67% - 99%), must be connected to the greenschist-facies metamorphism.
The geochemical data (
Foulde | Mako | Baniomba | |||||||
---|---|---|---|---|---|---|---|---|---|
basaltes M4 | Andesites M5 | Rhyolites M8 | Basaltes M3 | Andesites M2 | Rhyolites M2 | Basaltes M3 | Andesites M2 | Rhyolites M4 | |
SiO2 | 52.94 | 57.46 | 68.72 | 50.10 | 58.12 | 72.53 | 54.52 | 55.39 | 64.59 |
TiO2 | 0.70 | 0.71 | 0.41 | 0.78 | 0.96 | 0.54 | 0.70 | 0.70 | 0.43 |
Al2O3 | 13.21 | 15.19 | 14.73 | 12.38 | 16.34 | 12.94 | 13.81 | 14.21 | 13.64 |
Feo* | 10.27 | 8.40 | 3.86 | 10.24 | 8.77 | 4.56 | 9.74 | 9.08 | 4.29 |
MnO | 0.17 | 0.13 | 0.09 | 0.17 | 0.10 | 0.10 | 0.16 | 0.14 | 0.06 |
MgO | 8.88 | 5.29 | 2.21 | 9.57 | 3.36 | 0.99 | 6.64 | 5.63 | 3.76 |
CaO | 9.66 | 7.17 | 2.89 | 10.56 | 4.37 | 1.91 | 8.69 | 6.49 | 4.96 |
Na2O | 2.32 | 3.29 | 3.22 | 1.93 | 7.56 | 2.21 | 2.39 | 3.46 | 3.57 |
K2O | 1.24 | 2.14 | 2.77 | 1.31 | 0.27 | 2.73 | 2.37 | 2.31 | 0.70 |
P2O5 | 0.25 | 0.22 | 0.07 | 0.20 | 0.16 | 0.15 | 0.27 | 0.25 | 0.07 |
Rb | 37 | 58 | 104 | 38 | 6 | 85 | 170 | 64 | 24 |
Ba | 401 | 511 | 1976 | 356 | 80 | 424 | 775 | 714 | 244 |
Th | 1.69 | 2.05 | 7.588 | 0.98 | 1.05 | 4.605 | 1.36 | 1.85 | 1.5425 |
U | 0.74 | 0.80 | 1.68 | 0.39 | 0.40 | 0.80 | 0.61 | 0.63 | 0.55 |
Nb | 4.93 | 5.77 | 28.90 | 2.73 | 5.76 | 17.75 | 3.30 | 5.15 | 4.00 |
Ta | 0.20 | 0.30 | 1.22 | 0.17 | 0.45 | 1.30 | 0.20 | 0.35 | 0.35 |
La | 11.76 | 14.88 | 38.23 | 9.83 | 13.00 | 29.78 | 9.40 | 12.60 | 8.05 |
Ce | 26.47 | 32.24 | 82.29 | 24.07 | 28.97 | 63.28 | 21.20 | 26.25 | 16.50 |
Pr | 3.47 | 4.34 | 9.77 | 3.41 | 3.69 | 7.76 | 2.82 | 3.33 | 2.01 |
Sr | 517 | 506 | 337 | 409 | 166 | 104 | 576 | 349 | 348 |
Nd | 14.55 | 16.45 | 37.37 | 15.63 | 16.48 | 31.03 | 12.90 | 14.30 | 8.58 |
Sm | 3.75 | 3.66 | 7.49 | 3.76 | 3.76 | 6.45 | 3.14 | 3.39 | 2.02 |
Zr | 82 | 97 | 293 | 67 | 143 | 382 | 70 | 85 | 95 |
Hf | 2.10 | 2.50 | 5.95 | 1.90 | 3.60 | 8.20 | 1.80 | 2.35 | 2.63 |
Eu | 1.04 | 1.03 | 0.83 | 1.07 | 1.24 | 1.49 | 0.91 | 0.99 | 0.63 |
Gd | 3.88 | 3.60 | 6.50 | 3.56 | 4.13 | 6.45 | 3.05 | 3.33 | 1.97 |
Tb | 0.56 | 0.49 | 1.00 | 0.54 | 0.65 | 1.03 | 0.45 | 0.52 | 0.29 |
Dy | 3.04 | 2.87 | 5.87 | 3.10 | 4.23 | 6.52 | 2.68 | 3.15 | 1.61 |
Y | 18.53 | 16.89 | 39.15 | 17.43 | 26.48 | 40.27 | 15.10 | 17.75 | 8.80 |
Ho | 0.61 | 0.63 | 1.24 | 0.67 | 0.89 | 1.42 | 0.56 | 0.68 | 0.33 |
Er | 1.83 | 1.62 | 3.58 | 1.94 | 2.61 | 4.29 | 1.77 | 2.08 | 0.92 |
Tm | 0.24 | 0.27 | 0.51 | 0.27 | 0.38 | 0.66 | 0.23 | 0.29 | 0.13 |
Yb | 1.57 | 1.52 | 3.15 | 1.64 | 2.54 | 4.31 | 1.48 | 1.93 | 0.77 |
Lu | 0.28 | 0.26 | 0.47 | 0.26 | 0.41 | 0.71 | 0.23 | 0.31 | 0.12 |
Ni | 105 | 37.8 | 3.2 | 156 | 57 | 67 | 160.25 | ||
Cr | 666 | 203 | 9 | 740 | 420 | 215 | 240 | ||
V | 218 | 164 | 62 | 256 | 170 | 38 | 232 | 237 | 76 |
Co | 56 | 28 | 13 | 50 | 38 | 32 | 19 |
mobility during alteration and metamorphism. Alkalis (Na2O and K2O), too, which are reputedly mobile during post-magmatic phenomena reveal, in the facies examined, a noticeable increase with the rise of SiO2, despite the dispersion shown in the diagrams. In addition, the alkalis contents of these elements are not excessively high in the rocks, as they correspond to those found in calc-alkaline series. This observation rules out the hypothesis of an enrichment of these two oxides during the post-magmatic phenomenon. For all those reasons, we believe that these elements can be used in the discrimination diagrams.
To make a comparison between complexes, we considered the facies belonging to the same evolution stage, basing our study on the classification of Gelinas and Brooks [
The major elements data show a significant variation in the silica contents (50% to 78%) of the rocks from Foulde and Baniomba complexes. They also reveal TiO2, MnO and P2O5 almost invariably low contents (below 1%) in the rocks from all complexes; these contents decrease with the silica increase.
The MgO levels range from 0.2% to 11.4% and show a negative correlation with SiO2.
The CaO trend follows the MgO evolution, with contents ranging from 0.05% to 10.4%. The same phenomenon occurs for the FeO whose contents vary from 0.3% to 11.5%. The analysis of the geochemical data of major and trace elements allows us to conclude that the contents of MgO, CaO and FeO are generally high in basalts and andesites, but those contents must be related to the predominant ferromagnesian phases.
Na2O and K2O whose contents vary respectively from 1.05% to 4.3% and 0.11% to 4.21%, sometimes have high acid levels; they increase during differentiation.
Referring to the major elements in the Na2O + K2O − SiO2 classification diagram, the rocks studied are variously or unevenly distributed depending on the type of complexes (Figue 5). Thus, the Foulde calc-alkaline rocks include basalt, andesite, dacite/rhyodacite and rhyolite. This complex is the most differentiated one because it contains various rocks ranging from basalts to rhyolites. The Baniomba rocks are basalts, basalts/ande- sites, andesites and dacites, and the Mako rocks include basalts or andesites and rhyolites.
The Na2O + K2O − SiO2 diagram shows that the rocks examined belong to the subalkaline-type. This trend is confirmed by the iron, magnesium and alkaline contents that are compatible with the evolution of calc-alkaline formations.
Geochemical data of trace elements show the following: Chromium contents vary from 10 to 1032 ppm and show a
negative correlation with SiO2, and Co and V contents show the same evolution as Cr; their contents respectively range from 0.5 to 68 ppm and 6 - 271 ppm. Zr concentrations range from 60 - 177 ppm; and are quite high in acidic samples. They increase during differentiation.
Nickel, 96 ppm on average in basaltic rocks, shows concentrations lower than those of rocks from primary magmas that characteristically rise over 200 ppm (Sato, [
In basalts, the extension of the spectrum of rare earth elements (REE) to other trace elements doesn’t show a distinction between the three complexes. They have the same patterns (
U, Sr and sometimes in Ba (only for Foulde formations), and negative anomalies in Nb and Th. The overall for rare earths is 73.23 ppm for the Foulde basalts, 83.74 ppm for those of Mako, and 60.82 ppm for Baniomba basalts. The ratios (La/Yb)N are close to 4.15; 7.2; 4.28 respectively for the Foulde, Mako and Baniomba complexes. The ratios (La/Sm)N are close to 1.80; 1.96; 1.88 respectively and (Gd/Yb)N have values of 1.85; 2.21; 1.66 respectively for the Foulde, Mako and Baniomba basalts.
It is probably in the andesites (
For dacites and rhyodacites (
In Foulde and Mako, the ratio (La/Yb)N of rhyolites, like in the previous facies, is more pronounced (7.2 to 15.9) in Foulde, compared to Mako (4.6) (
Therefore, the spidergram of REEs extended to trace elements shows that the Foulde Group formations differ from those of the Mako Group regarding elements such as the extent of heavy rare earths (HREE), and the contents in Sr, Ba, Rb that are lithophile elements. The contents in these lithophile elements, which are very high in the andesites of the Foulde Group, reveal that the sedimentary environment has played a significant role in the formation of such rock.
The lithostructural map of the Mako Group (Diene, [
These basins are located between or inside greenstone panels (greenstone belts). In the Mako panel (
These basins expand from the North to the South and border the Greenstone Belt (
ü Border basins
They are located on the edge of greenstone panels. These basins surround greenstone belts and their limits are marked by NE-SW to N-S faults such as MTZ (Main Transcurrent Zone) and the Badon-Nienieko and Leoba- Moussala shear zone systems (Diene, [
These types of basin are common in deflection corridors. They represent real isoclinal folds suggesting dip- effect sedimentation, with detritic filling and heavily eroded high margins. These basins are somewhat overlapping
and are characterized by noticeable volcanism. The process of filling these basins will be completed by the debris from the erosion of the rocks that composed the high margins of greenstone panels, and by calc-alkaline volcanism as well. Inside those basins, the intermediate volcanism is especially marked by volcanic agglomerates evidencing sub-aerial volcanism which thus forms an andesitic complex. The lithology in the basins on the edge of the Mako Group consists, in its Southern part, in andesitic conglomerates that pass eastward to the Baniomba andesites (massive lava). In the northern parts, more specifically in the Foulde Group, the andesitic sequence could be equivalent to that of the southern part (Baniomba). These rock formations constitute an andesitic complex with volcano-detritic and volcanic features.
ü Type II basins
They are located within the first type of basins. Their sedimentation is different from that of dip-effect basins (type I) and they are imbedded in NE-SW and NS faults. This sedimentation is mainly composed of detritic metasediments but also of andesitic tuffs and gaps. The development of these basins may be caused by the system of North-South faults surrounded by NE-SW major faults such as the MTZ. These North-South faults may be transform faults that had replaced the sinistral displacements of NE-SW accidents, thus causing the formation of openings or basins within border basins.
The observation of the Mako Group lithostructural map (Diene, [
The structural evolution of the Mako Group is marked by two deformation phases that form a contunium: a tangential D1 phase that caused the crustal thickening and which is related to a horizontal shortening of the crust; this resulted in the formation of marginal basins; a D2-3 evolution characterized by transcurrent tectonics controlling the geometry and evolution of pull-apart basins (Diene et al., [
The high concentrations of transition elements (nickel, chromium, vanadium, cobalt) of magnesium, iron and calcium inside basaltic and andesitic rocks indicate the presence of ferromagnesian minerals. Thus, we can assume that these rocks originate from magmas resulting from the partial melting of the upper mantle, or from a richer source that contains these elements. Indeed, the rocks that compose the mantle are rich in minerals containing high concentrations of transition elements (olivine and pyroxene); the melting of such a rock can produce magmatic fluid enriched with these elements. This observation is compatible with the ratio values as (La/Yb)N, (La/Sm)N, (Gd/Yb)N and Al2O3/TiO2, which suggests the existence of a spinel Lherzolitic source or low-garnet source. The (La/Yb) ratios (1.36 to 4.12) are a strong argument for the involving of the melting of a lithospheric mantle source (El Hadi et al., [
Changes in silica contents and the presence of facies from basic to acid members evidence the differentiated nature of the magmas. The decrease of the concentration of some elements (nickel, chromium, cobalt, vanadium, iron, magnesium, calcium) from the least to the most differentiated rocks also shows the role played by the fractional crystallization that might be controlled by clinopyroxene and/or plagioclase fractionnation.
The origin of calc-alkaline Paleoproterozoic volcanic series from a unique magmatic source of either heterogeneous composition or not, could be considered as a defendable argument. This magma may have caused the formation of rocks developed at different times in the arc-basins, as a result of tectonic stresses.
Consequently, the magmatic source of the calc-alkaline series of Mako and Foulde complexes may be the same, but Mako’s belonging to the intra-block basin and Foulde to the pull-apart basin may have generated differences in the chemistry of CPX and in some trace elements. The Baniomba formations that had been developed in a marginal basin show intermediate characteristics.
In summary, based on some parameters such as the composition of the CPX and the trace elements contents, there apparently existed an evolution among the Mako formations that cropped out next to or inside the basic volcanic rocks of tholeiite-type from the Mako Group, the Foulde formations developed in a pull-apart basin and the Baniomba complex formations whose average compositions lied between those of Mako and Foulde.
The low contents in TiO2 and the high contents in lithophilic elements are in accordance with a development in an orogenic context. This orogenic environment is also confirmed by the Ti/V ratios below 40, very high Ba/Nb (El Hadi et al., [
The structural analysis indicates that contacts among lithological formations are tectonic in nature; they create intra-block basins (Mako), marginal basins on the edge of greenstones (Baniomba) and pull-apart basins (Foulde). The characteristics of their rocks are akin to each other regarding major and trace elements, but still, there exists a huge difference between the Ba, Sr, Rb contents and the U contents.
The three complexes of Mako and Foulde Groups containing calc-alkaline volcanic rocks of Paleoproterozoic- type are located from the North to the South of the Kedougou inlier. These complexes are composed of basic, intermediate and acid elements. The rocks show great similarities for major and trace elements, but they have some differences regarding certain lithophilic elements like Sr, Ba, U, Rb and the composition of Cpx. They probably originate from the same magmatic source; however, their development in such different environments as intra-block basins (Mako), marginal basins (Bagnomba) and pull-apart basins (Foulde) has presumably engendered some differences in their composition.
AdrienGozo,MahamadaneDiène,Dinna PathéDiallo,EdmondDioh,MamadouGueye,Papa MoussaNdiaye, (2015) Petrological and Structural Approach to Understanding the Mechanism of Formation and Development of Paleoproterozoic Calc-Alkaline Volcanic Rocks of West Africa’s Craton: An Example of the Mako and Foulde Groups (Kedougou Inlier in Western Senegal). International Journal of Geosciences,06,675-691. doi: 10.4236/ijg.2015.67055