The northwest of Côte d’Ivoire has been studied intending to reveal all the petrogeochemical characteristics and the tectono-metamorphic evolution of the lithological units
[1]
-
[3]
. The mapped lithological units are orthogneisses, quartzites with magnetites and amphibolites located to the west of Sassandra Shear Zone (SSZ) (Odienné region), which are, considered to be either ante-Eburnian rocks or early rocks in the Eburnian cycle
[3]
. For this author, the Eburnian volcanism of Odienné is characterised by the presence of a volcanic and volcano-sedimentary complex
[3]
[4]
. However, the Odienné area could be divided into three domains: (i) the western domain comprising metabasalts, metasediments, a volcanic complex (2.1 Ga) and deformed or undeformed plutons; (ii) the middle domain, which primarily consists of high-temperature paragneisses, mylonites, and ultramylonites; and (iii) the eastern domain comprising silico-clastic and volcaniclastic metasediments with anatectic conditions at the limit of the Tiémé batholith
[1]
. They concluded that these three domains were juxtaposed by horizontal movements, essentially senestial, sliding along the SSZ. Most of these volcano-sedimentary units are intruded by granitoids and dolerite dykes (or metabasites)
[1]
[3]
. Geochemical studies carried out in the northwest show that most of the metasediments in this zone correspond to siliceous metasediments, metapelites, and paragneisses derived from greywackes
[1]
[3]
. The West African Craton’s greenstone belt formations, which are rich in gold mineralization, are made up of a metasedimentary series associated with metavolcanic rocks that have been intruded by granitoids
[5]
. They are considered to be the hotter and deeper (15 km) portion of the Birimian crust, characterised by high-temperature prograde metamorphism with low-pressure anatexis (≈5 Kbars; 700˚ < T < 800˚)
[1]
. Furthermore, these metasediments and/or paragneisses of the central subdomain or SSZ are thought to have been emplaced in a vertical accretionary environment above a thinned ancient Archean crust
[1]
[6]
. The present research aims to ascertain the nature, origin, and emplacement context of the metasediments in northwest Côte d’Ivoire using petrographic and geochemical analysis. This detailed study of the metasediments in the northwest at the transition between the Kenema-Man nucleus (Archean) and the Paleoproterozoic belt of the Baoulé-Mossi domain contributes to a better understanding of the petrography, geochemistry, and emplacement conditions of northwest Côte d’Ivoire’s metasedimentary units.
2. Geological Setting
Côte d’Ivoire belongs to the West African Craton and more specifically to the Léo-Man ridge
[7]
-
[10]
(
Figure 1
). Its geology is mainly characterised by a basement of Precambrian age (Archean and Paleoproterozoic) which covers 97.5% of the territory and a recent sedimentary basin (secondary to Quaternary) covering the remaining 2.5% of this territory
[4]
(
Figure 2
).
The Archean domain is made up of ancient formations structured during the Leonian (3.4 - 3.0 Ga) and Liberian (2.9 - 2.7 Ma) orogenies
[6]
[11]
-
[16]
(
Figure 1
and
Figure 2
). It is characterised by two main groups including a basic complex essentially consisting of grey granulitic gneisses of the TTG type, migmatitic in places (first group), and a second group primarily made up of belts of supracrustal rocks
[12]
[17]
[18]
. Granites and charnockites are associated with these two groups either in the form of intrusions or as anatectic mobilisates
[8]
[14]
[19]
with an overprint of the Eburnian orogeny
[20]
-
[25]
. The term “quartzite complex” is used to designate supracrustal rocks composed of kinzigitic metasediments, magnetite quartzites, and granulitic basic rocks
[12]
.
Figure 1. Simplified geological map of the Léo-Man Dorsal (modified after <xref ref-type="bibr" rid="scirp.142820-34">
[34]
</xref> <xref ref-type="bibr" rid="scirp.142820-35">
[35]
</xref>). The Paleoproterozoic greenstone belts are divided into light green (volcaniclastic and intermediate to acid volcanic sediments) and dark green (intermediate volcanic lavas and products). SF or SSZ (Sassandra fault or Shear Zone), GFBF (Greenville-Ferkéssédougou-Bobo-Dioulasso Fault), HC (Haute Comoé basin), OF (Ouango-Fitini belt), Bu (Bui belt), Sw (Sefwi belt), Ba (Banfora belt), Bm (Bambéla basin) and Lw (Lawa belt) <xref ref-type="bibr" rid="scirp.142820-5">
[5]
</xref>.
The Paleoproterozoic domain, also known as the Baoulé-Mossi domain, lies to the east of the SSZ and encompasses the majority of the Ivorian Precambrian basement. Several investigations conducted in this area regarding its structuring have given rise to various controversies. Some work show that this structuring took place during the Eburnian megacycle (2.5 to 1.6 Ga;
[9]
[26]
[27]
) with tectono-metamorphic phenomena occurring between 2.2 Ga and 2.0 Ga
[28]
. However, others describe a division into two orogenic cycles, including the Burkinian (2.4 to 2.15 Ga), characterized by tangential tectonics, and the strict Eburnian (2.15 to 1.6 Ga)
[29]
. The Baoulé Mossi domain records ages between 2.4 and 1.8 Ga with juvenile formations and differentiation of the mantle, according to model ages between 2.5 Ga and 2.2 Ga
[30]
[31]
. The Birimian formations (greenstone belts and granito-gneissic areas) form grooves generally oriented NE-SW and also contain intrusive granitoids
[32]
. Between the Archean domain and longitude 6˚W, an Archean-Proterozoic transition domain is defined in Ivory Coast, characterized by negative neodymium epsilons, inherited zircons and Archean relics
[8]
. Finally, thanks to the thermobarometric study in the paragneisses (dated to the Archean), high-grade granulitic metamorphism was highlighted in the Paleoproterozoic domain of the SASCA sector or Sassandra-Cavally river sector (south of our study area)
[33]
.
Figure 2. Simplified geological map of Côte d’Ivoire, modified from <xref ref-type="bibr" rid="scirp.142820-9">
[9]
</xref>.
3. Methodologies3.1. Sampling
Several fieldworks studies have revealed eleven (11) metasediment outcrops in the Odienné, Touba and Séguéla regions. The process consisted of: (i) observing and describing the outcrops, followed by (ii) sampling a portion as a control and for future analysis. Various samples were observed and collected, including metaconglomerates, micaschists, migmatitic paragneisses and mylonitised quartzites, the coordinates of which are given in
Table 1
. These rocks are mainly affected by E-W and N-S to NW-SE structural deformation of the Sassandra Shear Zone (SSZ). We selected and described seven (7) samples, representative in terms of petrographic facies of the study area and for total rock geochemical analyses, in order to ensure good spatial coverage of the study area. Thin sections of the metasediments were prepared and studied under an Optika B-383POL polarising microscope coupled to a camera at the Geology and Mineral Resources Laboratory of the Université Félix Houphouët Boigny d’Abidjan-Cocody (Côte d’Ivoire). The acronyms used for the abbreviation of minerals are those of
[27]
.
3.2. Analytical Method
Geochemical analyses of major and trace elements (
Table 1
and
Table 2
) were carried out at the Bureau Veritas Canada laboratory. Major elements were determined by fluorescence spectrometry and trace elements by LA ICP-MS (Laser Ablation Inductively Coupled Plasma Mass Spectrometry) (
Table 1
and
Table 2
).
Loss on ignition (LOI1000 in %wt) was determined using a robotised TGA system (u351194_ABJ23001030;
https://www.bureauveritas.ci/
).
<xref ref-type="bibr" rid="scirp.142820-"></xref>Table 1. Geographic coordinates and geochemical data (major elements) for metasedimentary rocks in the north-western belt of Côte d’Ivoire.
Samples
OD064A
OD104
OD130
SEG017
OD184
OD154
OD220
OD221
OD203
TOU081
OD253
Lat
9.76841
9.32155
8.79326
8.1049966
9.31579
8.784607
9.337943
9.338803
9.313008
8.07891
10.19429
Long
−7.72265
−7.29574
−7.38403
−6.796107
−7.655202
−7.381868
−7.656923
−7.655191
−7.648182
−7.110866
−7.542159
SiO2
65.94
62.81
66.2
68.7
66.1
75.08
53.47
68.96
Al2O3
17.16
14.7
15.25
15.75
15.85
12.24
15.58
14.09
CaO
3.76
3.83
2.12
0.73
3.85
1.2
9.77
1.44
Fe2O3
3.9
7.11
5.71
2.59
5.25
3.85
8.77
4.45
K2O
1.79
3.37
2.46
7.46
3.03
1.91
1.35
3.01
MgO
1.47
3.1
2.48
1.16
1.42
0.61
5.05
1.58
Na2O
4.35
3.27
3.62
1.35
3.14
4.1
3.98
4.5
P2O5
0.153
0.197
0.152
0.152
0.156
0.064
0.21
0.145
SO3
0.198
0.084
0.392
0.027
0.009
0.107
−0.001
1.03
TiO2
0.4
0.65
0.53
0.52
0.6
0.27
0.86
0.38
MnO
0.04
0.12
0.07
0.04
0.13
0.13
0.2
0.08
Cl
0.002
−0.001
0.002
0.008
0.011
0.007
0.012
0.006
LOI1000
0.79
0.71
0.94
0.93
0.52
0.34
0.44
1.17
Total
100.23
100.25
100.09
99.72
100.25
100.04
99.89
101.13
CIA
63.41
58.40
65.68
62.28
62.93
61.27
50.78
61.15
K2O + Na2O
6.14
6.64
6.08
8.81
6.17
6.01
5.33
7.51
Log(SiO2/Al2O3)
0.58
0.63
0.64
0.64
0.62
0.79
0.54
0.69
Log(Fe2O3/K2O)
0.34
0.32
0.37
−0.46
0.24
0.30
0.81
0.17
DF 1
3.72
−0.67
−0.02
−8.22
1.59
0.36
4.32
−0.71
DF 2
2.48
0.45
−0.04
5.45
2.22
1.75
−1.27
2.94
K2O/Na2O
0.41
1.03
0.68
5.53
0.96
0.47
0.34
0.67
Al2O3/(CaO + Na2O + K2O)
1.73
1.40
1.86
1.65
1.58
1.70
1.03
1.57
<xref ref-type="bibr" rid="scirp.142820-"></xref>Table 2. Geochemical data (trace elements) for metasedimentary rocks in the north-western belt of Côte d’Ivoire.
Samples
OD064A
OD104
OD130
OD184
OD220
OD221
TOU081
Ag
−0.1
−0.1
0.2
−0.1
−0.1
0.2
−0.1
As
0.4
−0.2
506
0.4
0.6
3.0
0.4
Ba
928
1100
327
1640
761
305
1470
Be
1.6
1.6
1.2
4.2
2.0
1.2
2.0
Bi
0.04
0.08
0.76
0.06
0.02
0.1
0.14
Cd
0.2
0.1
−0.1
−0.1
0.2
0.7
−0.1
Ce
47.2
47.8
52.0
159
63.0
63.6
53.2
Co
7.8
22.4
41.3
3.3
7.1
2.5
12.5
Cr
36
165
139
5
2
5
51
Cs
4.14
3.31
2.51
4.0
4.84
3.12
0.63
Cu
16
52
66
12
16
32
18
Dy
1.36
3.14
2.75
4.95
7.82
7.49
2.11
Er
0.62
1.91
1.65
2.77
4.96
4.95
1.16
Eu
0.99
1.16
1.08
1.79
1.54
1.16
1.04
Ga
21.8
18.2
16.6
16.6
21.0
14.0
16.3
Gd
2.41
3.63
3.43
6.57
7.22
7.09
3.06
Hf
4.08
3.77
4.0
11.2
6.09
7.06
3.82
Ho
0.27
0.66
0.57
0.97
1.72
1.71
0.41
In
−0.05
−0.05
−0.05
−0.05
−0.05
0.05
−0.05
La
22.6
23.8
25.7
78.8
31.7
31.6
28.5
Lu
0.08
0.26
0.23
0.41
0.7
0.74
0.16
Mn
400
1050
652
305
968
936
543
Mo
0.6
0.8
2.8
2.8
0.4
1.0
1.8
Nb
7.12
8.08
6.9
31.1
13.0
14.4
7.95
Nd
21.6
22.9
23.6
61.8
33.1
31.2
23.1
Ni
16
64
70
−2
−2
10
14
Pb
8
10
5
21
9
68
11
Pr
5.78
5.96
6.32
18.6
8.31
8.06
6.37
Rb
62.2
109
94.6
265
86.4
58.4
77.5
Re
−0.01
−0.01
−0.01
−0.01
−0.01
−0.01
−0.01
Sb
−0.1
−0.1
1.2
0.2
1.4
1.6
−0.1
Sc
5.6
16.3
13.3
6.5
14.9
10.2
8.0
Se
−5
−5
−5
−5
−5
−5
−5
Sm
3.69
4.34
4.49
10.2
7.33
7.09
4.13
Sn
0.8
1.0
1.2
2.2
2.0
1.8
1.8
Sr
897
442
227
266
87.2
75.9
387
Ta
0.37
0.52
0.51
1.69
0.9
0.94
0.54
Tb
0.29
0.54
0.49
0.91
1.23
1.17
0.36
Te
−0.2
−0.2
−0.2
−0.2
−0.2
−0.2
−0.2
Th
4.39
4.65
5.67
24.2
7.19
8.31
5.65
Ti
2610
4190
3460
3060
3560
1610
2280
Tl
0.4
0.4
0.2
1.0
0.4
0.4
0.4
Tm
0.09
0.27
0.23
0.39
0.69
0.73
0.16
U
1.98
1.27
1.62
6.92
1.64
2.25
1.47
V
49.2
156
98.5
21.5
37.1
10.2
53.8
W
0.5
1.0
3.5
3.0
3.0
1.0
0.5
Y
6.9
17.1
15.2
26.0
47.0
43.1
10.9
Yb
0.6
1.83
1.58
2.83
4.86
5.06
1.18
Zn
85
65
30
40
75
215
35
Zr
150
135
146
474
228
257
135
Hg
Li
Ge
4. Results4.1. Petrographic Descriptions
The metasediments selected for this study are micaschists, paragneisses, and mylonitized quartzites located in two distinct metasedimentary units.
Most of the metasediments in the western sector are affected by EW-trending, sub-vertical, penetrative schistosity (
Figure 2
). Three micaschists are described in the metasediments located to the west of the SSZ.
Figure 3. Photography and microphotography (under transmitted light) of the metasediments. ((a), (b) and (c)): Outcrop and mineralogy of the mica meta-wacke; ((d) and (e)): Outcrop and mineralogy of the mica meta-wacke; ((f) and (g)): Outcrop and mineralogy of the garnet metawacke-litharenite. Quartz (Qz), Biotite (Bt), Feldspar (Fsp), Plagioclase (Pl), Microcline (Mcc), Chlorite (Chl), Muscovite (Ms), and Garnet (Grt); minerals’ abbreviations are according to <xref ref-type="bibr" rid="scirp.142820-27">
[27]
</xref>.
Most of the metasediments in this subdomain are affected by a penetrative schistosity oriented NS to NW-SE (
Figure 2
). Two-mica schists, paragneiss, and mylonite are described in the metasediments located within the SSZ.
Figure 4. Photography and microphotography (under transmitted light) of mica-schists (OD104 and OD130) and migmatitic paragneiss (OD064A): ((a) and (b)): Outcrop and mineralogy of sillimanite paragneiss; ((c) and (d)): Outcrop and mineralogy of micas meta-wacke; ((f) and (g)): Outcrop and mineralogy of amphibole micaschist. Quartz (Qz), Biotite (Bt), Feldspar (Fsp), Plagioclase (Pl), Microcline (Mcc), Chlorite (Chl), Muscovite (Ms), and Garnet (Grt); minerals’ abbreviations are according to <xref ref-type="bibr" rid="scirp.142820-27">
[27]
</xref>.
Figure 5. Photography and microphotography (under transmitted light) of the mylonite quartzite of the Sassandra River. Quartz (Qz), Biotite (Bt) and Feldspar (Fsp): minerals’ abbreviations are according to <xref ref-type="bibr" rid="scirp.142820-27">
[27]
</xref>.
4.2. Geochemical Data
The different concentrations of major and trace elements are recorded in
Table 1
. The SiO2 compositions of the metasediments are between 50.5% and 75.08%, with Al2O3 contents ranging between 12.24% and 17.16%. The alkali content (Na2O + K2O) is between 2.57% and 8.81%. The losses on ignition are quite low, around 1, except for the mylonite quartzite of the Sassandra River (TOU081), which is at 1.17%. The other major elements have the following proportions: Fe2O3 (3.85% - 13.75%); MgO (0.61% - 5.05%); CaO (0.73% - 9.7%); Na2O (0.67% - 4.5%); MnO (0.04% - 1.11%); K2O (1.79% - 7.47%); TiO2 (0.38% - 1.31%) and P2O5 (0.064% - 0.197%). The diagram in
Figure 6(a)
indicates that the rocks studied are of sedimentary origin with a well-marked peraluminous character
[10]
. Additionally, the diagrams in
Figure 6(b)
confirm this origin (
[36]
and
[37]
). According to the diagram in
Figure 6(c)
, the samples are mainly sandstones (wacke) and lith-arenites and incidentally shales
[38]
.
<p class="imgGroupCss_v"><img class=" imgMarkCss lazy" data-original="https://html.scirp.org/file/1211857-rId23.jpeg?20250526034547" /></p>Figure 6. (a) Discrimination diagram of <xref ref-type="bibr" rid="scirp.142820-10">
[10]
</xref>, (b) TiO<sub>2</sub> versus SiO<sub>2</sub> diagram of <xref ref-type="bibr" rid="scirp.142820-37">
[37]
</xref> and (c) Log (Na<sub>2</sub>O/K<sub>2</sub>O) versus Log (SiO<sub>2</sub>/Al<sub>2</sub>O<sub>3</sub>) diagram of <xref ref-type="bibr" rid="scirp.142820-38">
[38]
</xref> applied to metasediments from northwestern part of Côte d’Ivoire.
<p class="imgGroupCss_v"><img class=" imgMarkCss lazy" data-original="https://html.scirp.org/file/1211857-rId23.jpeg?20250526034547" /></p>Figure 6. (a) Discrimination diagram of <xref ref-type="bibr" rid="scirp.142820-10">
[10]
</xref>, (b) TiO<sub>2</sub> versus SiO<sub>2</sub> diagram of <xref ref-type="bibr" rid="scirp.142820-37">
[37]
</xref> and (c) Log (Na<sub>2</sub>O/K<sub>2</sub>O) versus Log (SiO<sub>2</sub>/Al<sub>2</sub>O<sub>3</sub>) diagram of <xref ref-type="bibr" rid="scirp.142820-38">
[38]
</xref> applied to metasediments from northwestern part of Côte d’Ivoire.
<p class="imgGroupCss_v"><img class=" imgMarkCss lazy" data-original="https://html.scirp.org/file/1211857-rId23.jpeg?20250526034547" /></p>Figure 6. (a) Discrimination diagram of <xref ref-type="bibr" rid="scirp.142820-10">
[10]
</xref>, (b) TiO<sub>2</sub> versus SiO<sub>2</sub> diagram of <xref ref-type="bibr" rid="scirp.142820-37">
[37]
</xref> and (c) Log (Na<sub>2</sub>O/K<sub>2</sub>O) versus Log (SiO<sub>2</sub>/Al<sub>2</sub>O<sub>3</sub>) diagram of <xref ref-type="bibr" rid="scirp.142820-38">
[38]
</xref> applied to metasediments from northwestern part of Côte d’Ivoire.
Figure 6. (a) Discrimination diagram of
[10]
, (b) TiO2 versus SiO2 diagram of
[37]
and (c) Log (Na2O/K2O) versus Log (SiO2/Al2O3) diagram of
[38]
applied to metasediments from northwestern part of Côte d’Ivoire.
The multi-element spectra of the western samples in green, and the SSZ in red, show slight and different variations (
Figure 7(a)
). The spectra of the incompatible lithophile elements or LILE (Ba, Rb, Th and U) show two isotopic trends: a positive anomaly (Ba and U), and a negative anomaly (Rb and Th) for the SSZ samples, while there is a negative Ba anomaly for those from the west (
Figure 7(a)
). The multi-element spectra normalized to the primitive mantle in
Figure 7(a)
, present remarkable negative anomalies in Nb, Ta, P and Ti
[39]
. Additionally, the negative anomalies in Ti and P of the whole spectra, may be due to the fractionation of ilmenite and apatite. These geochemical signatures are characteristic of magmas generated in subduction zones or from the melting of a pre-existing continental crust. Furthermore, the SSZ samples, compared to those from the west, show a very homogeneous appearance of these spectra and could reflect the signature of the same source, having fed their sediments at the same time (
Figure 7(a)
).
Figure 7. Multi-element (a) and rare earth (b) spectra applied to metasediments from the northwestern part of Côte d’Ivoire.
As for the rare earth or REE spectrum, all the samples evolve from lanthanum (La) to gadolinium (Gd) (
Figure 7(b)
). The spectra of the samples are characterized by a significant fractionation in LREE/HREE (
Figure 7(b)
). However, the rocks in the western part of the area, show a strongly negative anomaly in europium for its metasediments, while those located inside the SSZ, showing a very weak to almost zero anomaly in europium (
Figure 7(b)
). In addition, this negative anomaly in Eu, generally well-marked for the metasediments in the west and an enrichment in HREE unlike those of the SSZ, is typical of sediments of continental origin
[40]
.
The degree of alteration of the source rock can be assessed from the chemical index of alteration (CIA) based on the following molar proportions: CIA = [Al2O3/(Al2O3 + CaOσ + Na2O + K2O)] * 100 (CaOσ, corresponding to the concentration of CaO incorporated in the silicate fraction of the rock)
[41]
. Rocks with CIA values > 92 are highly altered due to the transformation of feldspars into clay minerals
[42]
. Rocks with CIA values between 60 and 80 show weathering, and those with CIA < 60 show, no or little weathering
[43]
[44]
. The studied samples have CIA values ranging from 50.78 - 65.03, indicating low weathering of sediments, resulting from the disintegration of the source rocks (
Figure 8(a)
). The index (CIA) associated with the ternary A-CN-K diagram, provides information on the intensity of the alteration as well as the composition of the original rock that gave rise to the sediments
[44]
. This index highlights a weak transformation of plagioclases into clays (
Figure 8(a)
). According to the ternary A-CN-K diagram coupled with the CIA index in
Figure 8(a)
, the metasediments of the Odienné and Touba regions would come from rocks with compositions between gabbros (basalt) and granites, and presenting a weak to moderate alteration
[41]
[45]
. The heterogeneous composition of the studied rocks is corroborated by the diagram (
[36]
), in which the samples show a distribution in the fields of sedimentary rocks (
Figure 6(a)
and
Figure 6(b)
).
Figure 8. (a) A-CN-K diagram of <xref ref-type="bibr" rid="scirp.142820-41">
[41]
</xref> <xref ref-type="bibr" rid="scirp.142820-45">
[45]
</xref> as a function of CIA = [Al<sub>2</sub>O<sub>3</sub>/(Al<sub>2</sub>O<sub>3</sub> + CaO* + Na<sub>2</sub>O + K<sub>2</sub>O)] × 100 of <xref ref-type="bibr" rid="scirp.142820-17">
[17]
</xref>, the variables are expressed in molar proportion and (b) Na<sub>2</sub>O/K<sub>2</sub>O diagram as a function of SiO<sub>2</sub> of <xref ref-type="bibr" rid="scirp.142820-5">
[5]
</xref> <xref ref-type="bibr" rid="scirp.142820-46">
[46]
</xref> applied to the metasediments of the northwestern part of Côte d’Ivoire.
Figure 8. (a) A-CN-K diagram of <xref ref-type="bibr" rid="scirp.142820-41">
[41]
</xref> <xref ref-type="bibr" rid="scirp.142820-45">
[45]
</xref> as a function of CIA = [Al<sub>2</sub>O<sub>3</sub>/(Al<sub>2</sub>O<sub>3</sub> + CaO* + Na<sub>2</sub>O + K<sub>2</sub>O)] × 100 of <xref ref-type="bibr" rid="scirp.142820-17">
[17]
</xref>, the variables are expressed in molar proportion and (b) Na<sub>2</sub>O/K<sub>2</sub>O diagram as a function of SiO<sub>2</sub> of <xref ref-type="bibr" rid="scirp.142820-5">
[5]
</xref> <xref ref-type="bibr" rid="scirp.142820-46">
[46]
</xref> applied to the metasediments of the northwestern part of Côte d’Ivoire.
Figure 8. (a) A-CN-K diagram of <xref ref-type="bibr" rid="scirp.142820-41">
[41]
</xref> <xref ref-type="bibr" rid="scirp.142820-45">
[45]
</xref> as a function of CIA = [Al<sub>2</sub>O<sub>3</sub>/(Al<sub>2</sub>O<sub>3</sub> + CaO* + Na<sub>2</sub>O + K<sub>2</sub>O)] × 100 of <xref ref-type="bibr" rid="scirp.142820-17">
[17]
</xref>, the variables are expressed in molar proportion and (b) Na<sub>2</sub>O/K<sub>2</sub>O diagram as a function of SiO<sub>2</sub> of <xref ref-type="bibr" rid="scirp.142820-5">
[5]
</xref> <xref ref-type="bibr" rid="scirp.142820-46">
[46]
</xref> applied to the metasediments of the northwestern part of Côte d’Ivoire.
Figure 8. (a) A-CN-K diagram of
[41]
[45]
as a function of CIA = [Al2O3/(Al2O3 + CaO* + Na2O + K2O)] × 100 of
[17]
, the variables are expressed in molar proportion and (b) Na2O/K2O diagram as a function of SiO2 of
[5]
[46]
applied to the metasediments of the northwestern part of Côte d’Ivoire.
Field data show an association of metasediments with metavolcanic rocks intruded by mafic, intermediate to felsic plutons. Most classifications related to metasediments highlight the existence of a correlation between the composition of detrital sediments and their geodynamic environments of deposition. Thus, the diagram in
Figure 8(b)
indicates that metasediments belong to three domains: the oceanic island arc margin domain, the active continental margin domain, and the passive margin domain
[46]
.
5. Discussion
The petrographic study of the metasediments in the north-western part of Côte d’Ivoire (Odienné and Touba regions) shows a diversity of rocks, the main ones being micaschists, quartzite-mylonites, and paragneisses. Paragneiss minerals include quartz, feldspar, biotite, sillimanite, tourmaline, and a few opaque minerals such as ilmenite. Micaschists are made up of quartz, biotite, garnet, plagioclase, amphibole, rare chlorite, and a few tourmalines and ilmenites. Finally, quartzite-mylonite is rich in quartz and feldspar, with some biotite. The presence of certain metamorphic minerals, such as sillimanite, confirmed the sedimentary origin of the samples. Most of these metasediments have shales and sandstones as their protolith. This study also showed a geodynamic environment of the oceanic island arc margin and an active to passive continental margin type for its metasediments. Work carried out in the study area shows the presence of paragneiss and micaschist with identical mineralogical assemblage, except for the presence of staurotide
[1]
. In addition, work carried out in the SASCA area (south-west Côte d’Ivoire; Comoé basin) also shows the presence of garnet, staurotide, sillimanite and cordierite paragneisses (
[47]
[48]
), and garnet and sillimanite paragneisses for the metasediments
[49]
. The estimated metamorphic conditions in our study area are amphibolite facies
[1]
. Some of these formations have also been observed in other birimian basins: Siguiri basin in Guinea (
[50]
[51]
), Cape Coast in Ghana (
[52]
), and Bandama in Côte d’Ivoire (
[53]
). Furthermore, the majority of Birimian basins are composed of sandstone and claystone
[42]
[52]
. The study area is thought to be made up of several small birimian basins
[54]
because the rocks studied are mainly composed of sandstones and lith-arenites. Furthermore, in our study area some others (
[1]
) indicate that the reworking or deformation of the pebbles could imply that the meta-conglomerates (OD253,
Figure 2
) represent the youngest terms of the sedimentary series to the northwest and that the Pb-Pb age on the zircons would be 2096 Ma obtained on a granitic pebble, representing the maximum limit of deposition
[28]
. Furthermore, new isotopic geochemistry data from Senegal show that Birimian rocks (Mako volcanic and Dialé-Daléma sedimentary) exhibit uniform juvenile characteristics with low initial Sr isotopic composition (0.700 to 0.704), positive Nd(t) values (2.1 to 4.3) and restricted Nd model ages (2.0 to 2.3 Ga)
[55]
. The triangular A-CN-K diagram of the rocks studied indicates that the protoliths evolve between basalts and granites (mixed volcanic and plutonic protoliths) after very little alteration (for sandstones) and little to moderate alteration (for shales) of the source rock indicated by the CIA alteration indices
[44]
-
[56]
. These results corroborate with certain works (
[1]
), which show an alteration and a recrystallization of the sediments of mafic to intermediate rocks for the biotite-amphibole-garnet micaschists in the western sector of Odienné. These results are similar to work on the Comoé basin, which reveals the existence of metasediments whose protoliths are thought to be intrusive (gabbros to granite)
[49]
[57]
. In addition, in the southwestern basin of Côte d’Ivoire, more precisely in the SASCA domain, the same protoliths are present with a smaller interval (basalt to andesite)
[47]
. The geotectonic environment of an oceanic island arc and/or active continental margin highlighted by the geochemical study of the metasediments studied is corroborated by several studies, including those of
[47]
-
[49]
[57]
. However, we have only one muscovite-rich metasediment seen on the western side of the SSZ (an area considered Archean to date), which falls within the field of passive margins. Only trace elements make it possible to distinguish the western domain from that of the SSZ in north-western of Côte d’Ivoire through Eu’s anomaly (
Figure 7
). These metasediments were probably generated in the Paleoproterozoic (Birimian). While some studies indicate that there were no plate tectonics during this period (
[58]
[59]
), various other studies stipulate that the Paleoproterozoic is more of a transition period in the evolution of crustal accretion processes
[8]
[60]
. Of course, the quantity of samples analysed by isotope geochemistry will not allow us to discuss the geotectonics, but they will give us an objective idea of the geodynamic conditions that prevailed in the north-western sector of Côte d’Ivoire. The geotectonic environments highlighted by this work may therefore be debatable. Indeed, future work will allow us to confirm or refute this geodynamic context and/or better understand the tectonic style in the northwest of Côte d’Ivoire.
6. Conclusion
This study, focusing on the metasediments of the northwest of Côte d’Ivoire (Archean-Paleoproterozoic transition domain), specifically in the localities of Odienné and Touba, contributes to improving the geological knowledge of this sector, which remains poorly known to date. The metasediments studied are composed of micaschists, paragneisses, and mylonite quartzites. The micaschists are distinguished by the following mineral assemblage: quartz, feldspars, garnet, and biotite. The paragneisses are also made up of sillimanite. The different classifications of these metasediments based on the major elements reveal a belonging to the group of sandstones with a small component of shales and lith-arenites. The alteration index (CIA) is low to medium, ranging from 50 to 65, indicating low atmospheric alteration of the source rocks that produced these metasediments, the protoliths of which could be basalts, andesites, granodiorites, and granites. It should be noted that the samples from the SSZ have higher CIA alteration index values, while those from other areas are rather low to moderate. Although debatable, the geodynamic environments of these metasediments are of the oceanic island arc margin and active and passive continental margin type. Field data show the presence of metasediments in the vicinity of metavolcamic rocks, all intruded by granitoids. All these rocks form units, greenstone belts in this region (fertile formations), whose in-depth study could highlight the presence of interesting indicators in terms of mineralisation.
Acknowledgements
This work is part of a doctoral study funded by the WAXI (West African eXploration Initiative) project in collaboration with the Agate project, the Geology and Mining Resources laboratory of the UFR STRM of the Félix Houphouët Boigny University of Cocody, Abidjan, Côte d’Ivoire and the LMI-MINERWA (Laboratoire Mixte Intermational-Laboratory for Responsible Mining in West Africa) project.
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