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The Birimian Granitoids of the Toumodi-Fetekro Belt in West African Craton (Côte d’Ivoire): Petrogenetic Overview and Link to Mineralization

T. K. Lionel-Dimitri Boya*, Martial P. K. Adingra, Allou Gnanzou, Gbele Ouattara, Apo Ryana L. Diane, Yacouba Coulibaly

Geology, Mineral and Energy Resources Laboratory, Training and Research Unit in Earth Sciences and Mineral Ressources, Félix HOUPHOUËT-BOIGNY University, Abidjan, Côte d’Ivoire

Abstract: The Toumodi-Fètêkro belt in Côte d'Ivoire is a one of its greenstone belts which has given rise to several mines in operation, with research or development work still in progress. This study based on a compilation of existing data acquired in different sectors, aims to contribute to the improvement of knowledge on the granitoids of this area. The geochemical data have therefore been reprocessed with a view to a global interpretation of the entire belt. Terranes are formed by granodiorites, granites, granophyres and tonalites with granodiorite and granophyres like host rocks. The peraluminous and metaluminous nature of magma shows that the granitoids come from mantle and crustal sources, with type I and S granites. The main anomalies noted indicate for these granitoids a character typical of volcanic arc magmas, an enrichment in K, or even a continental source. The deposits known in the Toumodi-Fètêkro belt are linked to several hydrothermal alterations. The control of the mineralization is litho-stuctural, with hydrothermalism being of major importance.

Keywords: petrogenetic synthesis, birimian granitoids, mineralization, Toumodi-Fetekro, Côte d’Ivoire

Received September 01, 2022; Revised October 02, 2022; Accepted October 10, 2022

Citation: T. K. Lionel-Dimitri Boya, Martial P. K. Adingra, Allou Gnanzou, Gbele Ouattara, Apo Ryana L. Diane, Yacouba Coulibaly, The Birimian Granitoids of the Toumodi-Fetekro Belt in West African Craton (Côte d’Ivoire): Petrogenetic Overview and Link to Mineralization. Journal of Geosciences and Geomatics, 10 (3). 139-152. January 2022. doi:10.12691/jgg-10-3-3

1. Introduction

Côte d'Ivoire belongs to the West African craton, precisely to the Man ridge. It is mostly constituted by a metamorphosed Precambrian basement, containing formations of lower Proterozoic age, known as birimian formations. These birimian formations contain deformed and elongated volcanosedimentary terrains, forming grooves or belts of greenstone, sometimes intruded by basin-type or belt-type granitoids. The Birimian formations are from Lower Proterozoic age, dated between 2150 and 1600 million years (Ma) [1,2,3,4,5].

These formations are structured in the form of rock belts of which 17 are counted in Côte d'Ivoire; they have the particularity of containing a large number of mineral substances of which gold is the most sought after. The Toumodi-Fètêkro belt, our study area, has been the subject of several studies, in particular some authors [6,7,8,9,10] who describe several lithologies. This paper will be particularly interested in the granitoids of this belt which often constitute the host rocks of mineralization. What are the petro-geochemical characteristics of the granitoids of the Toumodi-Fètêkro belt and what may be their link with mineralization?

The general objective of this study is to contribute to the improvement of knowledge on the geology of the Toumodi-Fètêkro Birimian belt. The specific objectives are to establish a petrographic synthesis of the granitoids, to carry out a comparative geochemical characterization; and highlight their relationship with the mineralization.

2. Geological Context

Côte d'Ivoire is located in the southern part of the West African Craton and in the southern part of the Man-Leo ridge (Figure 1). The territory has two geological units, a Precambrian basement that constitutes 97.5% of its territory and a sedimentary basin of 2.5%. The Precambrian basement is subdivided into two domains: the Kénéma-Man domain, which is located west of the Sassandra fault, where the geological formations are of Archean age, and the Baoulé-Mossi domain, which is located east of the Sassandra fault and is characterized by formations of Proterozoic age. The Kénéma-Man domain constitutes 20% of the basement and is formed of grey tonalitic and trondhjemitic gneisses, charnockites, metamorphosed green rocks in granulite facies, magnetite banded quartzites and biotite migmatites [11,12]; the Paleoproterozoic domain is characterized by the presence of volcanosedimentary rocks intercalated between granitoid batholiths. The structures of this domain result from tangential tectonics at the origin of N-S to NNE-SSW oriented structures [13] and transcurrent deformation, which is marked by the emplacement of large granitoid complexes around 2.1 Ga [14,15]. 17 ivorian greenstone belts are found in this domain, including the Toumodi-Fètêkro.

Figure 1. Schematic geological map of the Man-Leo Ridge, Kedougou-Kéniéba (KKI) and Kayes (KI) inliers [16]

This belt is located in Côte d'Ivoire and extends from south to north over an area of about 4908 km² and passes through the towns of Dabakala, Toumodi and Divo. The Toumodi-Fètêkro belt has within it birimian formations that contain deformed and elongated volcanosedimentary terrains, sometimes intruded by basin-type or belt-type granitoids (Figure 2).

Figure 2. Location in Côte d’Ivoire and geological map of the Toumodi-Fètêkro belt (extract from geological map of Côte d’Ivoire to 1/4000000)

3. Analytical Methods

The petrographic data were collected by previous authors from the preparation of thin sections of rock and their observation under a polarizing to identify the main minerals and the nature of the rock. The rock samples, transported to the analysis laboratory, were crushed and then pulverized before the analysis of their content in major elements by the X-ray fluorescence spectrometer, and in trace and rare earths elements by the inductively coupled plasma mass spectrometer (ICP-MS). In view of a global approach on the entire belt, we processed all the geochemical data (58 samples from south, center and north) using various diagrams: (i) Na₂O + K₂O (wt %) versus SiO₂ (wt %) classification diagram [17] to determine the nomenclature of granitoids, (ii) the discrimination diagram [18] to determine the type of granite (I or S) and the aluminous nature of the different granitoids, (iii) K₂O versus SiO₂ diagram [19] to determine the magmatic lineages or series of the granitoids studied and the particular tectonic environment of the setting up of the magma, and (iv) the multi-elements diagrams normalized to the primitive mantle to study the behavior and mobility of elements in the fusion liquid..

4. Results

4.1. Petrographic Data

The granitoids found in the belt are composed of granodiorites, granophyres, granites, tonalites, and microgranodiorites.

The granite, observed at Dougbafla, Toumodi and Bobosso is a leucocratic grainy rock, rich in plagioclase, quartz and microcline, with incidental muscovite, biotite and chlorite minerals as well as oxides. There is pseudomorphism of feldspars into epidote, sericite and carbonates [10]. The Dougbafla granite remains less widespread, with biotite often altering to chlorite, and accessory minerals such as apatite [9].

Granophyre, observed at Dougbafla, is a massive, leucocratic, fine-grained porphyry micrograin rock. It consists of phenocrysts of plagioclase, quartz, albite, muscovite and biotite. The accessory minerals are orthoclase, epidote and the metalliferous paragenesis is composed of magnetite, hematite, pyrite, arsenopyrite and pyrrhotite often accompanying gold

The tonalite, observed at Dougbafla, is a massive and grainy rock. It is composed mainly of plagioclase feldspars, quartz in various forms (micro-grains to macro-grains), calcite and biotite. The accessory minerals are apatite, chlorite and epidote.

Granodiorite, observed at Bonikro, Dougbafla, Toumodi and Bobosso is a massive grainy to grainy porphyritic, mesocratic rock, composed of very abundant plagioclase and/or microcline feldspars, quartz, amphibole, biotite, chlorite, sericite, epidote, albite and sphene. The presence of ferro-titanium oxides was noted [10].

Microgranodiorite, observed Dougbafla and Bobosso, is a massive homogeneous, mesocratic, micrograined rock, characterized by abundant phenocrysts of quartz in aggregates, orthoclase and plagioclase, biotite as well as chlorites, accompanied by sphene.

4.2. Geochemical Data

The results of the geochemical data are presented in the appendix. The geochemical studies have highlighted in the analyzed granitoid samples, relatively low contents of alkalis (Na₂O+K₂O) varying between 2.81% and 8.75%.

It has been noted too a diversity of compositions in these formations: mostly tonalitic, granodioritic and granitic, with some samples from the Center with quartz monzonitic composition and just only one sample from the South having a monzonitic composition (Figure 3). Moreover, three magmatic lines were highlighted: tholeic, calc-alkaline and shoshonite, with calk-alkaline dominance (Figure 4).

Figure 3. Na₂O+K₂O (wt %) versus SiO₂ (wt %) classification diagram [17] applied to Toumodi-Fètêkro belt granitoids

Figure 4. K₂O versus SiO₂ diagram [19] to the Toumodi-Fètêkro belt granitoids

The granitoids in south, center and north of the belt are predominantly I type (Figure 5). Only 3 samples in south from Dougbafla and 2 samples each from center and north are S type granite. S type granitoids show that the magma is derived from the melting of sediments while type I granitoids are derived from the melting of a crystalline rock from the mantle.

In south, center and north of the belt, the granitoids are peraluminous to meta-aluminous in composition (Figure 5), suggesting that the magmas that produced the protoliths are hybrid. These granitoids would thus come from crustal and mantle sources.

Figure 5. Discrimination diagram [18] applied to the granitoids of the Toumodi-Fètêkro belt

The Nb versus Y diagram [20] was used to investigate the geotectonic environment of the rocks (Figure 6). Because of their low Y content, all granitoids are found in the volcanic arc granite (VAG) fields and also fall within the syn-collisional granite (Syn-COLG) domain.

Figure 6. Trace elements discrimination diagram [20] Nb versus Y applied to granitoids

Multi-element spectra of the southern and central granitoids show negative anomalies in K, P and Ti while positive anomalies in Pb (which is a mobile element) are well marked in the northern granitoids and in U throughout the belt (Figure 7). Negative Nb and Th anomalies are found in south and center, and a negative Sr anomaly.

Figure 7. Multi-element spectra normalized to the primitive mantle applied to the granitoids (plutonites) of Toumodi-Fètêkro belt (A: southern part, B : central part, C : norther part)

Table 1. Summary of data on the various deposits in the Toumodi-Fètêkro belt

4.3. Mineralization

The prospects of all Toumodi-Fètêkro belt have hydrothermal alteration that has led to significant deposits. Most of these deposits are either hosted by granitoids, mainly granodiorites, or intruded by granitoids (plutonic or volcanic rocks). They are controlled by lithology or tectonics and have practically the same accompanying minerals (sulphides, calcite, hematite, pyrrhotite, arsenopyrite, chalcopyrite, dolomite and pyrite) except for the Bonikro deposit, whose gold-bearing paragenesis is composed of molybdenite, scheelite, tetradymite and sulphotellurides The 5 major deposits encountered in the belt are Agbahou, Bonikro, Dougbafla-Bandama, Bobosso and Lafigué from south to north, 4 of which (Bobosso excepted) led to mines in operation or under construction.

5. Discussion

Petrographic work carried out in the Toumodi-Fètêkro belt reveals a diversity of granitoids, especially in the center of the belt. They consist of granites, granodiorites and porphyroid granodiorites. Some first works [8] are confirmed by most recents studies [10] which described practically the same rocks in both the south and the center of the sillon. It has been noted an abundance of granite, granodiorite, porphyroid microgranite, granophyre and tonalite for granitoids in the northern part of the belt, in the Dabakala area and in its southern part, in the Oumé area located on the belt. In the northern part, some older studies [21] reported plutonic rocks, intrusive, discordant or concordant granodiorites and synkinematic granites sometimes with two micas. The Agbahou formations are composed of three lithological sets: volcanoplutonites, pyroclastites and metasediments, and discordant acid lava intrusions [6]. According to that, the first two sets would form the greenstone belt of the Oumé-Fètêkro chain, also known as Toumodi-Fètêkro belt.

Geochemical data show a diversity of compositions for the granitoids of Toumodi-Fètêkro furrow. Indeed, these formations are mostly granitic in composition, we could observe tonalitic, granodioritic with some quartz monzonitic sample compositions and a single sample of monzonitic composition in the South. This quartz monzonitic and monzonitic composition hadn’t been described in Bonikro [8], where granitoids are of three compositions, i.e. granitic, granodioritic and tonalitic. This work highlighted the monzonitic composition in southern part.

Three magmatic lineages were identified: (i) the calc-alkaline lineage observed in the majority of the granitoids, (ii) the shoshonitic lineage observed only in two samples, one from southern part and the other from central part, (iii) the tholeiitic lineage where are from four Dabakala samples and a sample from southern part. These results allow us to affirm that these granitoids would come from the same calc-alkaline magmatic lineage as the other granitoid samples.

These characteristics have already been reported for the granitoids of the Dabakala area in the north of the sillon and the Oumé-Hiré area in the south of the sillon. Indeed, the latter are all metaluminous to peraluminous, suggesting a hybrid source for these granitoids. This is what some works [7,9] have emphasized by evoking a dual origin (crustal and mantle) in the genesis of the granitoids.

Geochemical data also show that granitoids are derived from two geotectonic environments. Indeed, granitoids characterize both volcanic and syn-collisional arc environments, indicating their mantle sources with crustal components. This is consistent with a study [20] which states that granitoids in volcanic arcs have depleted mantle sources modified by a component of subducted oceanic crust and sediments and syn-collisional granitoids are characterized by pure crustal sources or by mantle sources containing large subducted crustal components

Excepted some rare samples which present a few differences in anomalies tendance, almost all granitoids in the Toumodi-Fètêkro belt are characterized by a positive zirconium anomaly, indicating a continental source [22]. Furthermore, the negative Nb anomalies are typical of subduction zone magmas [23]. Multi-element spectra normalized to the early mantle showed almost similar profiles in the south and center, slightly different from those in the northern part of the belt. Negative P and Ti anomalies are specifically noted in each part of the furrow, implying crystallization of apatite, ilmenite and titaniferous minerals in the melt, respectively. This also indicates crustal contamination in a mantle source, with potassium enrichment in these different rocks [24], expressed by the negative K anomaly. In addition, spider diagrams show positive Pb anomalies; Pb being a mobile element, it is taken up in the melt due to magmatic differentiation and radioactive decay of U to Pb. The negative Sr anomalies observed can be assimilated to a source change/modification or to the splitting of a phase [25]. The well-marked negative Th anomaly to the south and center of the furrow marks a lithological differentiation that may be of mining interest and potentially indicate the presence of ancient alterites (paleo laterites, [26]). Rare earths highlight differences between granitoids of the belt, a significant fractionation of rare earths in the Dabakala granitoids in the north has been noted while those of the southern and central granitoids is relatively low

Mineralization in all the deposits of the Toumodi-Fètêkro furrow is controlled by shear generating large shear corridors oriented along the birimian direction (N030-N035 and N040-50 SE). This induces hydrothermal fluids causing hydrothermal alteration with accompanying minerals mainly pyrite, pyrrhotite, arsenopyrite, chalcopyrite and sulfotellurides. Thus, mineralization seems to be associated with structural control.

Granitoids are represented throughout the Toumodi-Fètêkro belt, with some lithological variability. From one area to another, similarities have been noted, materialized among others by the presence of granodiorite and microgranite in the south, center and north of the belt. Differences were also noted, materialized by certain rocks observed only in certain zones; this is the case of granophyre observed to the north and south of the belt.

The presence of granitoids closely related to the mineralization has been noted: these are granodiorites, microgranodiorites and granophyres [7,8]. They are either in contact with the mineralized rock or in intrusion and carrying the mineralization themselves. Only the Agbahou deposit showed no apparent link with a granitoid [6]. This work has shown that granitoids are likely to contain significant mineralization; they can control mineralization and host an immense deposit. In the Toumodi-Fètêkro belt, several rocks are encountered, as in other Ivorian belts, but few have granitoids as host rocks or whose mineralization is controlled by granitoids.

This synthetic study shows a particularity of certain granitoids in the Toumodi-Fètêkro belt: they present a potential for gold mineralization, contrary to those of other Ivorian or West African birimic belt. The examples of deposits in the Mana district of Burkina Faso clearly shows that the host rocks for the mineralization are birimian greenstone belts and basaltic rocks, as well as those of Yaho (Houndé birimian belt) or the deposits.

6. Conclusion

At the end of this study on the granitoids of the Toumodi-Fètêkro belt, it appears that the granitoids contained in the whole belt have mostly similar characteristics, with some exceptions.

At the petrographic level, we can mention plutonic rocks (granodiorites, granites, tonalites) and vein rocks (microgranites and microgranodiorites).

A similarity can be seen between all the lithologies of the belt. The studied granitoids are peraluminous and metaluminous and come from two sources, namely mantle and crustal, with calc-alkaline to tholeic and shoshonitic affinities. They present a variability in their compositions: tonalitic, monzonitic, granitic and granodioritic. They are in the typical context of volcanic arc magmas and syn-collisional with two types of granites S and I.

The Nb, Ti and P anomalies show that these rocks are typical of volcanic arc magmas and indicate the crystallization of titaniferous minerals in the melt, a crustal contamination in a mantle source. Positive Pb anomaly indicates magmatic differentiation and radioactive decay of U to Pb and positive K anomalies indicate potassium enrichment. The zirconium anomaly highlights a continental source for granitoïds in the furrow, while Th anomaly indicates a mining interest and the presence of ancient alteration (paleo laterites).

At the level of mineralization, we have as host-rocks granodiorites and granophyres, then felsic intrusives which are in contact with basic materia. They are affected by deformations which favour the circulation of hydrothermal fluids with minerals such as chalcopyrite, pyrrhotite, arsenopyrite, hematite, dolomite and mainly pyrite.

Acknowledgements

We would like to thank the various collaborators who provided the data and assisted us in addressing our scientific concerns.

References

Appendix 1. Composition in major elements (%) and traces (ppm) of granodiorites and granites from the central part of the Toumodi-Fètêkro volcano-sedimentary furrow (Coulibaly, 2018)

Appendix 2. Major and trace element composition of the Bonikro granodiorites (Ouattara, 2015)

Appendix 3. Major and trace element composition of granodiorites from the Bonikro gold deposit (Ouattara, 2015)

Appendix 4. Chemical composition of granites and granophyres (Ouattara, 2018)

Annexe 5. Chemical composition of granodiorites and tonalites (Ouattara, 2018)

Appendix 6. Compositions of major (%) and traces (ppm) elements of plutonites from the Dabakala region (Gnanzou, 2014)

Appendix 7. Compositions of major (%) and traces (ppm) elements of plutonites from the Dabakala region (Gnanzou, 2014)

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