The Birimian Nassara volcanic formations are located south of Gaoua in the southern part of the Boromo belt. Within these formations is the Nassara gold deposit where mineralization is hosted at the contact between basaltic volcanic rocks and sedimentary rocks. It is with the aim of understanding the geodynamic context of the basaltic rocks and the implication of their primary gold potential in the Nassara gold deposit that this work is carried out. To achieve our objectives, 28 samples of fresh basaltic rocks were geochemically analyzed for their major and trace element compositions. These analyses show that the Nassara basalts are Fe-rich tholeiitic basalts. Rare earth profiles (La/SmN = 0.75 - 1.50; La/YbN = 0.65 - 2.18) are fairly flat and without europium anomaly (Eu/Eu* = 0.90 - 1.09), nor niobium. In the Zr/Nb vs. Nb/Th and Nb/Y vs. Zr/Y binary diagrams, the Fe-rich tholeiitic basalts of Nassara, as well as those of the Houndé and Boromo belts, are placed in the field of oceanic plateau basalts related to a mantle plume system. A gold fertility test carried out on these basalts was positive. As other studies have already shown, the genetic link between gold deposits and mantle plumes appears to be a general rule. The scenario for the Nassara gold deposit is that it is the source magma that was already more or less enriched in gold and other related elements on its way up. The remobilization of this gold would have occurred during the Eburnean orogeny with the help of metamorphic, hydrothermal and deformation phenomena to be redeposited at the level of shear zones with economic grades. Through this analysis, we show that the fertility of the initial lithologies is very important for the formation of economic size deposits in the proximal shear zones. Exploration work should now integrate this dimension to define the best targets.
The formations of the Man/Leo Ridge are organized into the Archean domain in the east and the Paleoproterozoic domain in the west (Figure 1). The Paleoproterozoic formations of the Baoulé-mossi domain are known as the Birimian formations [1]. These formations were emplaced around 2.1 Ga and represented a period of significant crustal accretion during the Eburnian orogeny [2].
In terms of geochemistry, it is generally agreed that the birimian formations are rocks related to rocks related to bimodal volcanism [3] - [8]. This bimodal volcanism is characterized by rocks with tholeiitic affinity and rocks with calc- alkaline affinity. The magmatism of the Upper Birimian calc-alkaline formations is related to intra-oceanic subduction zones evolving into an active continental margin (Lambert Smith et al., 2016). However, the geodynamic context of basalt emplacement remains a matter of debate. A first group proposes an island arc context [8] [9] [10] [11] [12]. A second group proposes a mantle plume context [3] [4] and finally the last group proposes a mid-ocean wrinkle context [13].
In the Houndé belt, tholeiitic basalts are emplaced in an oceanic shelf context [14]. In the Boromo and Houndébelts, [8] showed emplacement in an island
arc context. In the Guiana Craton, [15] showed that the El Calao basalts were emplaced in an oceanic plateau context for a mantle plume source.
Most orogenic gold deposits in the Man/Léo Ridge and in particular in Burkina Faso are contained in greenstone belts (Figure 2(a)). Many works have recently shown that the source of primary gold orogenic is related to the emplacement of intrusions, pyrite-rich carbonaceous sedimentary rocks and basaltic rocks [14] [15] [16]. Radiometric ages obtained from orogenic gold dating in different West African deposits show that the primary gold was emplaced between 2200 and 2120 Ma [17] and correspond to the major period of accretion of the Birimian formations around 2.25 to 1.98 Ga [2]. This coincidence shows that it was during the metamorphic and hydrothermal processes of the Eburnian orogeny that the primary gold was remobilized. The Boromo greenstone belt is known for its gold and base metal potential. These include the Poura, Konkéra, Torkéra and Nassara gold deposits, the Perkoa zinc deposit, and the Diénéméra-Gongondy copper porphyry.
The Nassara gold deposit located south of this belt is the subject of this study. The aim is to characterize the geodynamic setting of the Nassara gold deposit basalts and their primary gold potential. This study will be based mainly on geochemical analysis data on total rock (major and trace). These data will also be compared to other data obtained during previous work in the West African craton.
2. Regional Geological Setting
Like the entire Paleoproterozoic domain (Baoulé-Mossi domain) of the Man/Léo Ridge, in the Gaoua region, the Birimian formations are organized in greenstone belts formed essentially by a volcanic sequence and a volcano-sedimentary and sedimentary sequence representing the Birimian supergroup. At the limit of these greenstone belts are vast batholiths of tonalite, trondhjemite and granodiorite (TTG) which are syn-tectonic granitoids [19] [20]. The greenstone belts and batholiths (TTG) are later intruded by granitoids of various compositions, with calc-alkaline or alkaline affinity [18] [19] [21] [22] [23].
On the basis of lithostratigraphy, the Birimian supergroup consists of a lower birimian formed by ultrabasite, pillow lava basalt with tholeiitic affinity and andesites overlain by sediments. The upper birimian is dominated by sediments cut by basic to intermediate volcanic dykes with calc-alkaline affinity (dacite, rhyodacite, rhyolite). At its top is a thick detrital layer of sediment and carbonaceous rocks [5] [8] [24] [25] [26] [27] [28].
The Nassara gold prospect (Figure 2(b)) is located in the Boromo belt along the West Batié Shear Zone (WBSZ) south of Gaoua where the formations are essentially volcanic, volcanosedimentary and sedimentary rocks. The formations of the Nassara zone are essentially basalts, basaltic andesites, dacites, rhyodacites and granitoids. This ensemble is intersected by circumscribed intrusives of diorite and lamprophyre dykes [29]. These formations are affected by polyphase deformation throughout the Nassara Zone [29] [30].
3. Methodology
To carry out this work we collected core samples from different holes along the mineralized corridor. After microscopic observations, the freshest samples were taken for geochemical analysis. Samples were also collected from outcrops in the shear corridor. A set of twenty-eight (28) samples were selected, crushed for some and ground into a fine powder at the Geosciences and Environment Laboratory of Toulouse (GET). The powders of the different samples were conditioned in vials and labeled then sent for analysis. Major and trace elements were mainly measured by ICP-MS and ICP-AES at ALS (Spain). For more information you can visit the following website: https://www.alsglobal.com/.
4. Results
The Nassara basalts contain between 47.2 and 50.5 wt% SiO2, between 10.1 and 16.2 wt% Fe2O3, between 4.6 and 12.3 wt% MgO and 0.42 to 1.25 wt% TiO2. The different rock trends are recorded in Table 1. In the SiO2 Vs Zr/TiO2 * 0.0001 binary diagram of [31], the rocks confirm their basaltic nature (Figure 3).
Magmatic affinities tested for the Nassara basalts in the AFM diagram of [32] show that they have a highly iron-rich tholeiitic affinity (Figure 4), which is similar to the basalts of the Houndé and Boromo belts [8] [14]. Based on trace elements, we calculated Zr/Y ratios (Table 1). According to the work of Barrett
Representative major (wt%) and trace (ppm) element compositions for the Nassara basalts rocks
SAMPLE
Ba1
Ba2
Ba3
Ba4
Ba5
Ba6
Ba7
Ba8
Ba9
Ba10
Ba11
Ba12
Ba13
Ba14
Major elements (wt%)
SiO2
50
49.9
49.8
49.7
44
49.7
50.1
50.5
49.3
50.4
45.2
49.7
47.8
49.9
Al2O3
14
14.6
14.35
12.9
12.6
13.3
13.3
8.21
14.2
8.41
10.8
11.9
18.5
14.2
Fe2O3
13
13.4
14.55
15.2
12.9
15.2
15.3
10.8
14.5
10.9
10.3
11.9
10.6
13.8
CaO
11
10.1
10.75
10
8.42
6.63
6.55
14.3
10.8
14
9.53
10.5
13.4
10.4
MgO
7.8
7.37
5.32
6.25
4.23
6.34
6.4
12.3
6.05
12.3
8.04
9.24
5.54
6.58
Na2O
2
2.25
1.3
2.08
0.56
3.45
3.42
1.3
1.87
1.39
1.26
1.84
1.38
2.76
K2O
0.3
0.11
0.01
0.2
1.97
0.04
0.03
0.34
0.19
0.31
0.77
1.23
0.14
0.19
TiO2
0.8
0.98
1.2
1.06
1.11
1.18
1.22
0.42
0.94
0.42
0.5
0.63
0.63
0.88
MnO
0.2
0.19
0.2
0.22
0.16
0.21
0.21
0.21
0.21
0.21
0.16
0.2
0.16
0.22
P2O5
0.1
0.09
0.17
0.1
0.11
0.11
0.12
0.08
0.08
0.08
0.12
0.17
0.05
0.07
LOI
2.7
2.85
3.81
2.72
14.2
3.87
3.82
2.23
2.35
2.23
12.8
3.32
2.17
1.17
total
102
101
101.5
100.5
100.3
100.2
100.6
100.9
100.6
100.7
99.6
100.7
100.4
100.2
Traces elements (ppm)
Ba
107
27.6
12.8
110
170
30
30
280
30
270
160
380
30
40
Ce
7.8
8.7
14.7
10.8
13.2
8.4
8.6
6.4
9.7
6.2
9.1
11.2
4.9
6.8
Cr
540
280
190
110
70
100
100
720
110
730
340
390
200
180
Cs
0.5
0.27
0.14
0.2
2.7
0.4
0.4
0.3
0
0.3
2.6
0.5
0.2
0.2
Dy
3.2
3.81
5.47
4.55
4.3
4.83
4.92
1.94
3.94
1.94
2.04
2.6
2.47
3.43
Er
2.1
2.49
4.11
2.92
2.73
3.38
3.33
1.22
2.57
1.31
1.36
1.61
1.69
2.27
Eu
0.7
0.8
1.3
0.97
0.93
0.93
1.03
0.51
0.86
0.49
0.54
0.66
0.6
0.68
Ga
15
16.1
19
16
16
16
16
9
16
9
11
12
15
15
Gd
2.7
3.2
4.72
3.57
3.52
3.66
3.77
1.75
3.02
1.78
1.98
2.31
2
2.73
Hf
1.6
1.9
2.8
2
2
2
2
0
2
0
0
1
0
1
Ho
0.7
0.8
1.24
0.95
0.93
1.06
1.09
0.4
0.83
0.42
0.42
0.55
0.53
0.73
La
3
3.2
5.8
4.2
5.1
3.2
3.2
2.7
3.6
2.8
3.8
4.8
1.8
2.5
Lu
0.3
0.39
0.6
0.42
0.39
0.49
0.47
0.17
0.35
0.17
0.18
0.22
0.25
0.33
Nb
2.5
2.4
5.9
3
Nd
5.7
6.8
10.2
8.4
9.6
7.4
7.3
4.8
7.1
4.9
6.1
7.4
4.2
5.8
Pr
1.2
1.36
2.14
1.62
1.89
1.36
1.37
0.94
1.49
0.95
1.27
1.57
0.76
1.07
Rb
7.3
2.7
0.2
4.5
48.6
1
1
4.6
3.3
4.6
30.8
24.6
2.7
2.7
Sm
1.9
2.26
3.37
2.7
2.8
2.6
2.5
1.4
2.4
1.3
1.7
2
1.4
1.9
Sr
143
185
194
130
100
230
230
380
170
400
280
310
150
80
Tb
0.5
0.56
0.82
0.64
0.63
0.69
0.7
0.29
0.58
0.3
0.32
0.37
0.36
0.5
Th
0.3
0.22
0.43
0.6
0.6
0.4
0.3
0.4
0.4
0.4
0.5
0.7
0.2
0.3
Tl
0.5
0.5
0.5
0.66
0.67
0.72
0.72
0.26
0.58
0.27
0.31
0.37
0.38
0.52
Tm
0.3
0.35
0.61
0.43
0.41
0.49
0.48
0.17
0.36
0.18
0.18
0.24
0.25
0.34
U
0.2
0.07
0.14
0.11
0.22
0.09
0.09
0.19
0.11
0.18
0.27
0.34
0.07
0.07
V
322
363
297
363
325
368
361
248
327
247
240
269
232
311
Y
19
22.4
34.6
24
22.5
25.2
25.5
10.1
19.8
10.2
10.8
13
13.5
18.4
Yb
2.2
2.48
3.91
2.7
2.6
3.1
3.1
1.2
2.4
1.2
1.2
1.5
1.6
2.2
Zr
51
56
91
69.2
71.7
60.4
58.4
27.3
64.5
32.1
31.7
35
33.1
44.7
Co
49
48
44
54.8
48.6
51.6
52.6
49.7
54.5
50.5
41.6
44.5
42.7
51.9
Cu
183
150
157
180
150
130
120
50
150
40
120
100
110
140
Ni
162
146
85
85
59
78
71
81
89
81
55
59
105
101
Zr/Y
2.68
2.5
2.63
2.88
3.18
2.39
2.29
2.7
3.25
3.14
2.93
2.69
2.45
2.42
Zr/Nb
20.4
23.33
15.42
23.06
Nb/Th
8.33
10.90
13.72
5
Nb/Y
0.13
0.10
0.17
0.12
Eu/Eu*
0.94
0.91
0.99
0.95
0.95
0.90
0.92
1.02
0.99
0.97
0.98
0.90
0.94
1.09
(La/Yb)N
0.93
0.88
1.01
0.97
1.06
1.33
0.70
0.70
1.53
1.02
1.59
2.16
2.18
0.77
(La/Sm)N
0.99
0.89
1.08
0.82
0.97
1.14
0.77
0.80
1.21
0.94
1.35
1.40
1.50
0.81
Au
-
-
-
3
44
0
0
0
0
2
5
0
1
0
and maclean (1999), ratios < 4 correspond to a tholeiitic affinity, ratios > 7 show a calc-alkaline affinity. Ratios between these two values correspond to a transition lineage. For the Nassara basalts, the values are between 2.03 and 2.67 confirming their tholeiitic affinity. This character is confirmed in the diagram of [33], where the Nassara basalts like other Paleoproterozoic basalts of the West African craton [8] [13] are placed in the tholeiitic field (Figure 5). The Nassara basalts are highly Fe-rich tholeiites.
In the diagram of [34], the rare earth spectra (Figure 6) normalized to chondrite (La/SmN = 0.75 - 1.50; La/YbN = 0.65 - 2.18) are flat with no significant europium anomaly (Eu/Eu* = 0.90 - 1.09) suggesting little or no plagioclase fractionation. By these characters, the Nassara basalts show similarities to those of the West African craton oceanic shelves [13] [14], to those of the Pacific oceanic plateaus [35] (Figure 7). In the trace element spider diagram [36] normalized to the early mantle (Figure 8), a flat spectrum is observed for high field strength
elements (HFSE) except for Ti where a negative anomaly is observed; the absence of a niobium anomaly suggests that there is no crustal contamination. The slight negative anomaly in titanium reflects a slight fractionation of the oxides. The variation of the Sr anomaly, sometimes positive and sometimes negative, the negative Rb anomaly, and the negative K anomaly suggest a slight hydrothermal alteration.
5. Discussion
The geodynamic context of the West African Craton (WAC) basaltic formations is defined by two groups of authors. A first group of authors [6] [8] [9] [10] [11]
[12] propose that the WAC basalts formed in a mid-ocean rift context or in an island arc context. The second group of authors proposes an oceanic shelf context with mantle plume activity [3] [4] [13] [14] [37] [38]. [13] defined three types of tholeiites for the WAC formations ranging from PTH1 to PTH3. For the geodynamic setting, he proposes an oceanic basin formed by subsidence.
In what follows, the geochemical characteristics of the Nassara basalts compared to similar materials in the West African craton and worldwide will be discussed in turn. These include the geodynamic context of emplacement, the source of the magma, possible crustal contamination of the magma, and their possible implication as the source of the primary gold.
5.1. Implications for Tectonic Setting
According to [39], island arc basalts have a niobiom (Nb) content of less than 2 ppm. and thus [40] discriminated mid-ocean rift basalts (MORB) with an Nb content < 3 ppm and ocean plateau basalts (OPB) with an Nb content > 5 ppm. Another boundary between the two types of basalts [40] is based on the La/Nb ratio. MORBs have a La/Nb ratio > 1.4 and La/Nb values < 1.4 are unique to oceanic shelf basalts. [15] also relied on niobium content to discriminate Paleoproterozoic basalts from El calao as ocean plateau basalts.
Analytical data for the Nassara basalts show that the niobiom content is between 2 - 5.9, and La/Nb ratios between 0.9 and 1.4 are also less than or equal to 1.4. The flat rare-earth spectra without significant europium anomaly show low fractionations (La/SmCN = 0.75 - 1.14; La/YbCN = 0.65 - 1.22). All these characteristics allow us to say that the Nassara basalts were emplaced in an oceanic plateau context.
5.2. Mantle Source
A discriminating argument to show the mantle origin of the magmas is the use of Nb/Th-Zr/Nb and Zr/Y-Nb/Y diagrams, because these elements are incompatible in the mantle. The position of our data in the Nb/Th-Zr/Nb and Zr/Y-Nb/Y diagrams [41] [42] (Figure 9 & Figure 10) shows that they are mantle-sourced
magma that would have been emplaced in an oceanic plateau environment as a mantle plume. In the WAC, similar emplacement contexts in mantle-sourced oceanic shelf environments have already been proposed for tholeiitic basalts [3] [4] [13].
Work by [42] has also shown that relationships between elements such as Zr-Y-Nb-Th provide useful geochemical fingerprints for distinguishing mantle plume head and tail. For the Nassara case, this may well be a mantle plume head source for the Nassara basalts. In addition, the source of the parental magma can be distinguished on the basis of MgO content [43]. For example, they define for the tail of the plume magnesium-rich komatiitic rocks, for the central part of the plume magnesian komatiites and for the head of the plume weakly magnesian komatiites.
On this basis, we can say that the composition of the Fe-rich Nassara tholeiitic basalts corresponds to a plume head origin probably from its peripheral part. Another alternative proposed as sources of the Paleoproterozoic iron-rich tholeiites named PHT1 and PHT2 [13] is that of partial mantle melting at depth.
5.3. Crustal Contamination
Geochemical data from the Nassara Zone basalts do not show a negative Nb anomaly, characteristic of crustal contamination. This observation has already been made by a number of previous works based on isotopic data, suggesting the juvenile character of the Paleoproterozoic crust of the West African craton [3] [4] [10] [20] [25] [27] [36]. Furthermore, the La/SmN ratio of 0.75 to 1.14 (<1.5) of the Nassara Zone basalts supports the idea of a mantle magma that has not undergone contamination [44].
5.4. Implications for Gold Sources
The Nassara basalts, which were emplaced in an oceanic plateau setting as a mantle plume, are believed to be fertile in gold from the source magma that was more or less enriched in gold and other related elements on its way up. This was confirmed by the fertility test performed on samples not affected by hydrothermalism taken outside the mineralized corridor. Indeed, it is shown that most large orogenic gold deposits and large gold provinces are related to mantle plume activity that generally favors lithospheric growth in an active continental margin setting [14] [15] [45] [46] [47] [48] [49].
This predisposition is probably due to the fact that the source of the mantle plumes can originate from the core-mantle boundary and thus transport the gold-enriched material upward [50]. These same authors believe that hot mantle activity in contact with the crust causes devolatilization and melting of the crust which is a precursor for large orogenic gold deposits.
The Nassara gold deposit is thought to be due to remobilization of primary gold from basalts by metamorphic and hydrothermal processes and its deposition in low pressure zones created by contemporary tectonics during the Eburnian orogeny. This interpretation is in agreement with the work of [48] and [51] who shows that orogenic deposits are located in shear zones as a result of metamorphic processes. In relation to this remobilization issue, [52] estimated that 19 km3 of tholeiitic basalts with 1 ppb of primary mineralization is required to form a 1Moz gold deposit.
In the West African Craton and in particular in the Man/Leo Ridge, recent work has shown by the Re-Os method that orogenic-type gold mineralization contained in the shear zones is between the period of 2150 Ma and 2085 Ma ± 71 Ma [17]. These same authors dated the gold mineralization at Nassara to 2094 ± 58 Ma. This age could be interpreted as the age of the metamorphic and hydrothermal processes that led to the remobilization of the primary gold and the emplacement of the Nassara gold deposit. Numerous works [29] [53] among others) have shown that large gold deposits developed at the contact between tholeiitic basalts and sedimentary rocks. The contact zones are indeed zones of weakness that are borrowed by the transcurrent shear that creates the dilatant structures able to channel the hydrothermal fluids that have circulated in the fertile basalts.
6. Conclusions
Major and trace element geochemical data allowed us to characterize the Nassara basalts as iron-rich tholeiitic basalts. They are also marked by fairly flat profiles through the rare earth elements normalized to chondrite and through the High field strength elements (HFSE) of trace elements normalized to the primitive mantle. The Zr/Nb vs. Nb/Th and Nb/Y vs. Zr/Y binary diagrams show that the Nassara Zone basalts were emplaced in an oceanic shelf setting emanating from a mantle plume. These basalts are the primary source of mineralization for the Nassara gold deposit. This gold was remobilized during metamorphic and hydrothermal processes and redeposited in shear zones.
This study shows that it is important to perform a rock fertility test in a mining exploration area to have the best chance of success.
Acknowledgements
This work is a part of the PhD thesis work that I defended in 2019 at Joseph KI ZERBO University. The authors want to thank the mining company B2Gold, through its chief geologist Mr. NARE Athanase for allowing us to sample the different rocks for the analyses. The WAXI-2 project funded the field work and geochemical analyses. The Institute of Research for Development (IRD) for its logistic support.
Conflicts of Interest
The authors declare that there is no conflict of interest with this paper.
Cite this paper
Ouiya, P., Yaméogo, A.O., Ilboudo, H. and Naba, S. (2022) Implication of Paleoproterozoic Basalt Fertility Related to Mantle Plume Activity in Nassara Gold Mineralization (Burkina Faso, West Africa). Open Journal of Geology, 12, 1013-1031. https://doi.org/10.4236/ojg.2022.1211048
Appendix. Supplementary Geochemical Analyses of Nassara Basalts
Representative major (wt%) and trace (ppm) element compositions for the Nassara basaltic rocks.
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