4.1.1. Metasediments

1)Mica schist

The widely distributed schists (32% of the total) are always in an advanced state of weathering and mainly contain sericite and pyrite, sometimes in significant quantities. These schists may be enriched with sandy elements (mainly quartz). They are traversed by large quartz veins, which are often gold-bearing. Originally grayish to greenish-gray, they give rise to outcrops of laterites that have retained their original schistosity, or yellow and brown clays with whitish, reddish, and purplish streaks. Rare outcrops of fresh mica schist have nevertheless been observed near the towns of Dimbokro and Ahua (Figure 3(a)). The schistosity affecting the rock is oriented NE-SW and dips to the northwest. In thin sections, the rock has a grano-lepidoblastic texture highlighted by mineral foliation with alternating surmicacous beds and quartz-feldspar beds. The surmicacous beds consist of brown biotite, sometimes chloritized (green biotite), and muscovite, accompanied by interstitial crystals of xenomorphic quartz (Figure 3(b)).

2)Metagraywacke

Metagraywackes are observed in the bed of the N’Zi River in the village of Broukro, where they form alignments of sometimes thin bands (Figure 3(c)). To the naked eye, the rock is dense, very coherent, dark in color, schistose in appearance, and generally derived from sandstones with relatively abundant cement (20%). Under the microscope, samples taken from the matrix, which have a granolepidoblastic texture dominated by the orientation and interlocking of phyllitic minerals, show the following mineralogical composition (Figure 3(d)): Quartz constitutes the bulk of the rock, often with very frequent and intense rolling extinction, indicating strong deformation. Micas (muscovite and biotite) are very abundant, forming elongated aggregates and continuous bands that align clearly to define the foliation. Chlorite is often associated with the alteration of biotite. Plagioclase crystals are less abundant than quartz and are generally unaltered. Opaque minerals are accessory minerals in the slide, appearing as small, scattered opaque black grains, probably iron oxides. The composition of these metagrauwackes, a mixture of quartz, feldspars, and micas in a fine matrix, is consistent with that of Birimian grauwackes described in other basins in the region [13][11].

3)Quartzite

Macroscopically, this rock appears as a beige-grayish to white block with a massive, granular appearance (Figure 3(e)). The texture is clearly granular, with grains visible to the naked eye, suggesting recrystallization. Under the microscope, the rock has a granoblastic texture, characterized by an overwhelming dominance of quartz (Figure 3(f)). The quartz grains are medium to coarse in size, generally xenomorphic to subautomorphic in shape, and show rolling extinctions and mechanical twins, evidence of the deformation undergone during metamorphism. The grain joints are sutured and interlocked, indicating complete recrystallization of the original sediment. Accessory minerals are present in very small quantities, appearing as fine colored (yellow, orange, brown) or opaque patches scattered between the quartz grains. These traces of oxides may correspond to minute amounts of clays or iron oxides present in the sedimentary protolith (pure quartz sandstone) prior to metamorphism.

Figure 3.Macroscopic and microscopic aspects: Mica schist. (a) and (b); Metagraywacke (c) and (d); Quartzite (e) and (f). Qz: quartz. Pl: plagioclase. Bt: biotite. Mu: muscovite. Chl: chlorite. Op: opaque.

4.1.2. Nature and Origin of Metasediments

The chemical compositions of the seven samples analyzed are presented in (Table 1). SiO₂ contents vary between 62.8% and 87.6%, with the highest values in quartzites (DIM2-1: 87.6%) and the lowest in mica schists and metagrauwackes. Al₂O₃ contents ranged from 6.3% to 17.5%, with the highest values found in the mica-rich mica schists (DIM5 and DIM6). Fe₂O₃ concentrations ranged from 2.88% to 7.04%. CaO contents are generally low (0.08% to 3.21%), with the exception of sample DIM3 (3.21%), which also has a high MgO content (3.40%). This last sample could reflect a higher proportion of ferromagnesian minerals or carbonates in the protolith. Alkalies (Na₂O + K₂O) vary between 1.74% and 6.70%, with a K₂O/Na₂O ratio between 0.41 and 5.21. Loss on ignition (LOI) is moderate (1.2 to 2.6% for most samples), with the exception of DIM6 (LOI ≈ 0.02%), which reflects hydration linked to the presence of phyllitic minerals.

The [17] diagram (Figure 4(a)) indicates that all samples fall within the range of sedimentary rocks with a meta-aluminous to peraluminous character, consistent with protoliths of pelitic to greywackeous composition. According to [18] classification diagram: Log (Fe₂O₃/K₂O) as a function of Log (SiO₂/Al₂O₃) (Figure 4(b)), the samples are mainly distributed in the shale and wacke fields. Only one sample (DIM2-1) is positioned in the quartzarenite field, consistent with its dominant quartz content (SiO₂ = 87.6%). This distribution is characteristic of sediments in Birimian basins, where shales and grauwackes coexist with subordinate sandstone levels [9][11].

The chemical weathering index (CWI = [Al₂O₃/(Al₂O₃ + CaO* + Na₂O + K₂O)] × 100; [19] was calculated for each sample. The values obtained range from 54.3 to 79.1, indicating low to moderate alteration of the source rocks. The highest values (DIM2-1: 79.1; DIM2: 66.4; DIM5: 66.8) correspond to samples richer in Al and poorer in CaO + Na₂O, indicating more advanced hydrolysis of feldspars in the source rock or longer transport of detrital material. The lower values (DIM3: 54.3; DIM6: 57.6) suggest a less altered source, probably slightly to moderately transformed igneous rocks.

Figure 4.(a) [17] discrimination diagram; (b) Log (Fe₂O₃/K₂O) versus log (SiO₂/Al₂O₃) diagram [18]; (c) A-CN-K diagram; (d) Chondrite normalized rare earth spectra and (e) Multi-element diagrams of metasedimentary rocks normalised to the primitive mantle [21] applied to metasediments from the Dimbokro region.

The A-CN-K ternary diagram (A = Al₂O₃, CN = CaO + Na₂O, K = K₂O, in molar proportions) by [20] (Figure 4(c)) indicates that the protoliths of the studied metasediments range from granodiorites and granites. The alteration trajectory of the samples is consistent with an evolution from source rocks of intermediate to felsic composition, slightly to moderately altered.

The rare-earth spectra [21] (Figure 4(d)) of the Dimbokro metasediments show a marked enrichment in light rare earth elements (LREE) relative to heavy rare earth elements (HREE), with (La/Yb) N ratios ranging from 7.2 to 18.6. The mica schists exhibit the most pronounced fractionation, indicating a source dominated by felsic crustal materials, whilst the metagrauwacks, with more moderate values, reveal a more significant contribution from a mafic volcanic source. The europium anomaly is slightly negative for the majority of samples (Eu/Eu*: 0.67 - 0.95), indicating a source that has undergone plagioclase differentiation, typical of Eburonian granitoids and TTGs. Only sample DIM6, with a positive anomaly (Eu/Eu* ≈ 1.12) and high MgO and TiO₂ contents, stands out due to a greater contribution from a mafic source to the cumulate. Overall, these spectra confirm a mixed sedimentary supply from intermediate to felsic crustal sources of arc affinity, within the context of the Eburnean orogeny.

The multi-element spectra normalized to the primitive mantle of [21] (Figure 4(e)) show profiles that are generally consistent with each other. There is a relative enrichment in elements with large ionic radii (LILE: Rb, Ba, K) and a marked depletion in elements with high ionic charges (HFSE: Nb, Ta, Ti). This depletion in Nb-Ta relative to La, Th, and Ce is characteristic of magmas and sediments derived from sources linked to a subduction zone [3][22]. The positive Ba anomaly (particularly in DIM3: 1176 ppm) may be linked to a high detrital component of potassium feldspars, or to diagenetic processes. The rare earth elements show little differentiation between LREE and HREE, with La/Yb (N) values ranging from approximately 10 to 25, suggesting a continental crustal source.

4.1.3. Geotectonic Environment of Metasediments

The K₂O/Na₂O diagram as a function of SiO₂ by [23] (Figure 5) is used to discriminate the geotectonic environment of detrital sediment deposition. In this diagram, the Dimbokro samples are distributed between the fields of the oceanic island arc margin and the active continental margin. This bipartition is consistent with the results obtained in other areas of the Comoé Basin [24] and in comparable Birimian basins in Ghana [11][25].

Figure 5.K₂O/Na₂O discrimination diagram based on SiO₂ in the geotectonic context of metasediments, according to [23].

The negative Nb-Ta anomaly observed in the multi-element spectra reinforces this interpretation. It indicates that the sediments were supplied, at least in part, by igneous rocks associated with an arc or active margin context, rather than an oceanic ridge or hotspot context [26][27].

4.2.1. Petrographic Data

1)Biotite granite

These are fairly dark-coloured, medium-grained granites (Figure 6(a)). They are much more widespread within the study area and are mostly calcic. They outcrop as small massifs shaped by foliation to the south-west of Ebimlossou and at Dida Mouessou, along the Dimbokro-Bocanda axis, where they form a sacred heritage site. Their textural characteristics and their map boundaries intersecting the overlying strata suggest a syn- to post-S2 emplacement. Microscopic examination reveals plagioclase, sometimes zoned with a more calcic and retromorphosed core, as well as quartz in xenomorphic patches with undulating extinction. Biotite is the main ferromagnesian mineral, forming brown lamellae exhibiting marked pleochroism (brown to brown-green). The alteration phases include chlorite and epidote (pistachite) resulting from the alteration of biotite, sericitisation of the alteration products of the plagioclases, and zircon (pleochroic halo in the biotites) (Figure 6(b)).

Figure 6.Macroscopic and microscopic aspects: Biotite granite (a) and (b); Granodiorite (c) and (d); Tonalite (e) and (f). Qz: quartz. Pl: plagioclase. Bt: biotite. Mu: muscovite. Hbl: hornblende; Chl: chlorite; Ser: sericite; Op: opaque.

2)Granodiorite

These relatively rare facies consist of medium- to coarse-grained rocks (Figure 6(c)). Thin-section analysis reveals a distinct granular texture with a dominant percentage of plagioclase. The plagioclase is more or less retromorphosed (sometimes zoned) and its composition varies from oligoclase to andesine. Microcline occurs either as interstitial material, in small crystals, or as rare phenocrysts. Quartz forms xenomorphic patches with rolling extinction. In natural light, biotite, in large automorphic crystals, is greenish-brown in colour. Rare hornblende crystals have occasionally been observed. Accessory minerals include chlorite, epidote resulting from the destabilisation of biotite, and sericite from the alteration of plagioclases (Figure 6(d)).

3)Tonalite

The only tonalite massif has been identified in the central-eastern part of the study area (Figure 6(e)). It is dark grey in colour and has a medium to fine grain. At the microscopic level, we observe that microcline is absent or very rare (always less than 3%), compared to the dominant plagioclase (oligoclase). Quartz (over 20%) crystallises in large xenomorphic patches. Green biotite sometimes forms clusters, and there are rare sections of amphibole in the form of elongated greenish prisms. Among the accessory minerals, of note is the local presence of sulphides within the classic suite of accessory minerals (pistachite, chlorite) (Figure 6(f)).

4.2.2. Nature and Origin of Granitoids

The major element compositions of the seven samples are shown in Table 1. SiO₂ contents range from 61.51% to 73.2%, with higher values for biotite granites (72.9% - 73.2%) and progressively lower values for granodiorites (66.1% - 68.4%) and tonalites (61.51% - 62.08%). The Al₂O₃ contents are relatively stable (14.2% - 16.1%); those of Fe₂O₃ and MgO increase steadily from granites to tonalites, reflecting the overall more mafic composition of the latter. The low TiO₂ values (0.11% - 0.55%) are characteristic of magmatic arc plutonites [28].

In the (Na₂O + K₂O) vs SiO₂ diagram by [29]. (Figure 7(a)), the samples are distributed across the fields of granites, granodiorites and tonalites, in perfect agreement with the field petrographic nomenclature. The diagram by [30] indicates that almost all the samples belong to the sub-alkaline series (Figure 7(b)). In diagram [31], the rocks are mainly situated in the peraluminous zone (Figure 7(c)). The diagram by [17], confirms that these granitoids from the Dimbokro region are of type I, consistent with their petrographic characteristics (presence of amphibole, mafic inclusions, Na₂O/K₂O ratio generally greater than 1 in the tonalites and granodiorites) (Figure 7(d)).

The rare-earth spectra, normalised to chondrites according to [27], show a profile with a moderate to steep negative slope, with a marked enrichment in light rare earth elements (LREE) relative to heavy rare earth elements (HREE). The (La/Yb) N ratios vary between approximately 15 and 110 depending on the sample, reflecting varying degrees of fractionation within the suite. The Eu anomaly is generally weak to absent (Eu/Eu* close to 1 for most samples), suggesting that plagioclase was not a dominant residual phase in the source, or that it did not accumulate significantly during crystallisation. Sample DIM2-2, which is distinguished by particularly high total rare earth element (REE) contents and a strong positive Eu anomaly, may have undergone local enrichment linked to plagioclase accumulation or the introduction of late-stage fluids (Figure 8(a)).

Figure 7.(a) Classification diagram from [29]; (b) Diagram of [30]; (c) Diagram of [31] and (d) Diagram of [17] applied to the granitoids from the Dimbokro region.

Multi-element diagrams normalised to the primitive mantle show, for all samples, a systematic enrichment in large-ion-radius elements (LILE: Cs, Rb, K, Ba) associated with negative anomalies in Nb, Ta, P and Ti. These anomalies in HFSE (high-ion-radius elements) are typical of magmas generated in subduction zones [1][32]. The negative anomalies in Ti are attributable to the early fractionation of ilmenite and/or sphene in the parent magma (Figure 8(b)).

4.2.3. Geotectonic Environment of Granitoids

In order to understand the geotectonic context of the emplacement of the Dimbokro granitoids, the geochemical data were plotted on the Ta vs Yb discriminant diagram by [33]. All samples fall within the volcanic arc granitoids (VAG) field, with the exception of a few points located on the boundary with the syn-collisional granites (Syn-COLG) field. This distribution is consistent with a subduction setting, likely within an active continental margin or an island arc above a subducted plate (Figure 9).

Figure 8.Chondrite normalized rare earth spectra and primitive mantle normalized multi-element spectra applied to plutonites from the Dimbokro region.