The internal domain is composed by three distinct palaeoproterozoic units [8] [11] (Figure 3): 1) the Loémé Unit outcropping in the southern part of the belt. It is composed of schists, ortho and para gneiss intruded by the Bilinga and Bilala metagranitoids whose ages U-Pb on zircon, ID-TIMS are respectively 2048 ±

12 Ma and 2014 ± 56 Ma [8] [16] and U/Pb on zircon, SIMS age is 2028 ± 12 Ma [11]; 2) the Loukoula Unit outcropping in the northern part of the belt contains para and orthogneiss, micaschists, schists, amphibolites and quartzites cut locally by Les Saras granodiorite plutons and dolerite dykes. Les Saras granodiorite yielded U/Pb zircon age of 1920 ± 10 Ma, TE-TIMS [17] and 2000 ± 80 Ma, ID-TIMS [5], and 2038 ± 10 Ma, SIMS [11]; 3) the Bikossi Unit is composed essentially by quartzite and contains locally conglomeratic level, micaschists, schists and amphibolites [3] [4] [8] [10] [11] [15].

Detrital zircon geochronology in the quartzite yielded age of sources between 2.20 Ga to 2.00 Ga [8] and 3.08 Ga to 2.04 Ga [11]. This unit is cut by Mont Kanda and Mfoubou granites which yield respectively ages of 928 to 932, U-Pb zircon, LA-ICP-MS [11] and 1050 ± 25 Ma, U-Pb zircon, ID-TIMS [16].

In the Araçuaï belt in Brazil, the internal domain is represented by the paleo-mesoproterozoic Espinhaço Supergroup composed of vulcanite, quartz-sandstone, conglomerate, pelite, and subordinate carbonate [18] [19] [20] deposited at around 1.75 Ga [21].

The intermediate domain is represented by the lower part of the west congolian Supergroup [6] [11] (Figure 3). It comprises: 1) the Sounda Group containing the Nemba Complex Subgroup composed of metagabbros, metabasalts, amphibolites and greenschists and dated at 915 ± 8 Ma, U-Pb zircon [11]. Similar basic magmatic rocks, the Gangila basic rocks of the Zadinian Group in RD Congo yielded age comprise between 999 ± 7 Ma and 920 ± 8 Ma. [6]. The metabasite rocks of the Nemba Complex are considered derived from tholeiitic lava flows containing pillow structures [15] or a continental tholeiitic rift magma [11] [14]; 2) the Kakamoeka Subgroup, or Mayumbian Group of RD Congo, composed of conglomerates, quartzites, graphitic schists, ignimbrites, rhyolites, tuffs, metabasic rocks and yielded age between 920 ± 8 Ma and 912 ± 7 Ma [6]; 3) the Mvouti Subgroup constituted of chlorito-schists, ampelitics schists, quartzites, meta-sandstones and meta-arkoses; 4) the Moussouva Subgroup composed of quartzites and schists. The lower part of west congolian Supergroup is considered as an aulacogen deposit [4] or a syn-rift sequences [11].

The external domain is represented by the upper west congolian Supergroup (Figure 3). It comprises the lower Diamictite (or Tillite) composed by glaciogenic [3] [4] [8] [22] or a mud flow deposits [2] [11] [23] constituted by black calcareous shale containing heterogeneous, heterometric and heteromorphic pebbles and boulders. An intercalation of basic magmatic rocks is described in RD Congo. It is underlaid by the Louila Subgroup composed of meta-sandstones, locally conglomeratic, quartzites, quartzo-schists and schists with intercalation of limestones and calcschists [3] [4] [8] [11] [22]. The Louila formation is overcome by the glacio-marine upper Diamictite formation [4] of marinoan age [24]. In the top, the Schisto-calcaire Group made of thick carbonated platform deposits [3] [23] [25] [26] [27] contains shales and siltstones intercalations and his folded outcrops area constituted the transitional zone with the subtabular deposits of the Niari-Nyanga basin. The upper west congolian Supergroup is considered as a passive margin deposit [11].

In Araçuaï orogen, neoproterozoic sediments is represented by the Macaubas Group whose age is situated between 1000 Ma and 850 Ma [28] [29]. The sediments took place in rift basin which evolved into an arrow ocean basin [30]. The Macaubas Group contains in the lower part a tillite (or diamictite), sandstones, pelites, and subordinate basic volcanics. It passes in the east and south of the belt to thick sequences of distal pelites with intercalations of sandy turbidites [29] [31] and an ophiolitic assemblage, composed of basalt, chert, banded-iron formation, gabbro, plagiogranite, and ultramafics rocks. Mafic rocks of the assemblage yield a Sm-Nd isochron age of 816 ± 72 Ma (with εNd = +3.8), interpreted as the time of magmatic crystallization [32].

The deformation and the metamorphism in the Mayombe belt decrease from the internal domain to the external domain. They whole domains are affected by thrust faults with northeast vergence.

In the intermediate and external domains two deformations phases oriented roughly NW-SE are observed. The first phase in the west of the intermediate domain is marked by isoclinal folds with an eastern vergence and penetrative cleavage schistosity (S₁) and become right folds in the external domain. The second phase is characterized by right fold slightly verged bearing a strong crenulation schistosity (S₂) in the intermediate domain. This crenulation schistosity (S₂) becomes discrete in the external domain. These two phases of deformation are attributed to panafrican events [4] [5] [8] [10] [11] [33].

The metamorphism is amphibolite facies in internal domain [10] [11] [12] and decrease to greenschists facies in the intermediate domain and passes to anchizone facies in the external domain at the limit of the Niari-Nyanga basin [11].

In the internal domain, the palaeoproterozoic basement is affected by strong crenulation schistosity (S₂) oriented NW-SE which refolds paragneissic foliation [4] [8] [10] [11] [12] [33]. Locally crenulation schistosity (S₃) oriented NE-SW is described in Loeme unit [4]. The foliation of paleoproterozoic formation is attributed to eburnean event [4] [10] [11] [12] and the crenulation schistosity (S₂) is from panafrican event [4] [12].

The samples are collected at the western part of the Mayombe belt (Figure 2) in the Loukounga River near the Mbéna area. This zone is characterized by the passage of paleoproterozoic unit to neoproterozoic formations. Basics samples collected are attributed to Neoproterozoic Nemba Complex. Fine sections of selected samples for petrological determination are confectioned in laboratory of the fine sections of University of Rennes 2, France.

Geochemical analyses of major, trace and rare earth elements were done to evaluate the petrogenesis of rocks. Major, trace and rare earth elements were determined on selection samples without sign of weathering and/or a slight hydrothermal overprint. Samples are powdered and placed in fusion with LiBO₂ and dilute by HNO₃ and performed by inductively coupled plasma-mass spectrometry (ICP-MS) and inductively coupled plasma atomic emission spectrometry (ICP-OES) in the “Centre de Recherches Pétrographique et Géochimique” (CRPG) of Nancy, France. The quality control is realized with international geostandards.

The rock outcrops along the Loukounga river and are made of paragneiss, micaschists amphibolites, metagabbros, and greenschists (Figure 4).

Paragneiss (Figure 4(a)) are composed of an alternating millimetric to centimetric rich biotite levels and rich quartzo-feldspathic levels. They are attributed to paleoproterozoic unit which constituted the basement of the Mayombe belt. Amphibolites (Figure 4(a)) are found locally in contact with paleoproterozoic paragneiss of Loukoula unit. In some places they are massive but are generally strongly deformed with cleavage schistosity (S₁) and discrete crenulation schistosity (S₂) and shows right fold accompanied of thrusting movement (Figure 4(b)). Metagabbros (Figure 4(c)) are in massive lenticular corps surrounded by fine matrix made of greenschist. Micaschists (Figure 4(d)) are in alternation with chloritoschists and bear crenulation schistosity. The whole rocks are locally affected by quartz and calcite veins that run parallel to the schistosity.

Metabasites rocks of Loukounga are studied on fine sections and some examples presented in Figure 5.

Metagabbros are represented by samples Louk 30b (Figure 5(e)) and Louk 32 (Figure 5(f)). They are made of actinote, hornblende, epidote, plagioclase, sphene, pyroxene, zircon and rare opaque. The pyroxenes are pseudomorphozed on green amphibole which line plagioclase crystals relics. Plagioclases are often saussuritized on epidote and locally contain epidote, quartz and calcite intrusions. The textures are varied from nematogranoblatic, lepidogranoblastic to lepidoblastic.

Epidotites are made of pistachite, plagioclase, chlorite, biotite, pyroxene, actinote and opaque minerals (Figure 5(g), Figure 5(h)) in variable proportions. They contain veins or amygdales composed of epidote, quartz, calcite and chloritized biotite, often oriented along schistosity. Epidote is either in fine crystals either in porphyroclastes moulded in the schistosity. The textures observed are

granoblastic and grano-lepidoblastic and in some places it becomes mylonite type.

26 samples from metabasites of Loukounga are analysed and their results presented in Table 1. Major elements give value SiO₂ (41.85% - 58.23%), Al₂O₃ (13.35% - 19.14%), MgO (2.03% - 7.11%), CaO (4.13% - 12.61%), Na₂O (0.45% - 6.68%) and TiO₂ (1.07% - 2.69%).

The Mg# colour index [34] is comprised between 16.2% and 43.6%. The TiO₂ concentration based of [35] [36] and [37] classifications give 19 samples with low Ti (TiO < 2) and 6 samples with high Ti (TiO > 2).

The Harker diagrams (Figure 6) of mobile elements as Na, K, LILE, and Pb used to detect influence of weathering or low-grade metamorphism in the samples show a bad correlation between major and traces elements. In contrast, the high field strength elements (HFSE) relatively motionless define linear trends in binary element diagrams.

Zr/Ti-Nb/Y diagram of [38] modified by [39] (Figure 7) place samples in basalts and andesitic basalts fields. The Zr/Y < 4.5 ratio of the greenschists and epidotites indicate a tholeiitic basalt and the Zr/Y > 4.5 ratio of the amphibolites and metagabbros place the rocks in transitional basalt. The Nb/Y < 1.0 ratio correspond of that of a subalkaline rock.

The composition of incompatibles traces elements is illustrated in binary

diagrams normalized to chondrites and primitive mantle (Figure 8). Rare earth spectra of Loukounga lava normalized to Nakamura [40] chondrites (Figure 8(a)) are subparallel in shape at HREE and slightly concave downwards at MREE and some samples show weak negative Eu anomalies (Eu/Eu* = 0.83 - 0.99) and others on the other hand showing more positive anomalies in Eu (Eu/Eu* = 1.01 - 1.11). All samples are enriched in LREE and are characterized by steeper REE slopes than E-MORB (LaN/YbN: 3.67 à 6.77). Total REE concentrations are consistently higher in all lavas than MORBs (∑REE: 78.85 à 264.60).

The normalized spectrum to the N-MORB of [41] (Figure 8(b)) is marked by a selective enrichment in LILE (Cs, Ba, Sr) compared to HSFE (Zr, Nb, Th, Y) and contains a strong positive Pb anomaly and a negative Nb, K, Zr and Ti anomalies. The normalized spectrum to the primitive mantle of [42] shows enrichment in LILE and HFSE elements (Figure 8(c)). The anomaly is slightly negative for Ta-Nb and Ti and strongly positive for Pb.

Traces elements are used to determine geological context. The Zr/Y-Zr diagram of Pearce and Norry [43] place the rocks in within plate basaltic lavas, except two rocks which located to the limit of MORB field (Figure 9). The Zr/Y > 1.5 attribute the rocks to continental types of Pearce [44].

Zr-Th-Nb triangular diagram of Wood [45] and Nb-Zr-Y triangular diagram of Meschede [46] place samples in wide fields from the MORB, WPT, CAB and Alkaline basalt to arc basalt (Figure 10).

Plotted in Th/Ta-Tb/Ta diagram of [47] [48] used on the metabasites rocks of the Mayombe of Gabon, samples are concentrated in CFB field (Figure 11).

Plotted in Th/Ta-Tb/Ta diagram of [47] [48] used on the metabasites rocks of the Mayombe of Gabon, samples are concentrated in CFB field (Figure 11).

Metabasites samples of Loukounga are ranged macroscopically in amphibolites, metagabbros epidotites and greenschists facies. Fine sections show a hydrothermal overprint marked by: 1) a zoned vacuoles filled with epidote, quartz and chlorite which successively crystallized; 2) an amygdale filled by calcite; 3) a late secondary growth of non-oriented epidote, chlorite, hornblende and quartz over older parageneses (Figure 5).

Geochemical of major elements shows that these rocks are basic to intermediate composition with a few samples in ultrabasic composition. The Mg# colour index [34] value indicated that they are in part felsic with differentiated magma and in part mafic with poorly differentiated magma. The Harker diagrams (Figure 6) show a bad correlation between major and traces elements. In contrast, the high field strength elements (HFSE) relatively motionless define linear trends in binary element diagrams indicating that their concentrations have not been affected by weathering or low-grade metamorphism.

Samples in discrimination diagrams Zr/Ti-Nb/Y of [38] modified by [39] characterized samples as basalts and andesitic basalts fields (Figure 7). The Zr/Y < 4.5 ratio of the greenschists and epidotites indicate a tholeiitic basalt and the Zr/Y > 4.5 ratio of the amphibolites and metagabbros place the rocks in transitional basalt. The Nb/Y < 1.0 ratio correspond of that of a subalcalin rocks.

Spectra of Loukounga normalized to N-MORBS and primitive mantle [41] (Figure 8(b)) show enrichment in LILE and HFSE elements but with slight negative anomalies for the Nb, Ta and Ti and Sr variables anomalies. Positive anomaly is very strong for Pb, this confer a tholeiites continental character. It is comparable to those known elsewhere as in the traps of Decan [49] and Frankelin (Figure 12) [50].

The Zr/Y-Zr diagram of [43] places the rocks in within plate basaltic lavas, except two (02) rocks one of which is in the field of MORB (Figure 9). A tholeiitic basalts origin is detected for greenschists and epidotites with Zr/Y < 4.5, however a transitional basalts origin is considered for amphibolites and metagabbros with Zr/Y > 4.5. The Zr/Y > 1.5 attribute the rocks to continental types of [41].

Within intraplate basalts associated with E-MORB and Calco-alkaline Basalt are detected in triangular (Zr-Th-Nb) diagram of [45] (Figure 10(a)). The E-MORB associated with major samples plotted in alkaline basalt and arc basalt is recognized in triangular (Nb-Zr-Y) diagram of [46] (Figure 10(b)). The wide dispersion from within plaque basalt (WPB) to arc basalt fields is often characteristics of continental within plaque basalts particularly the traps basalts or CFB [51] like observed in Th/Ta-Tb/Ta diagram of [47] [48] (Figure 11) used for the metabasites rocks of the Mayombe belt in Gabon.

CFB-related lavas belong to an association of transitional tholeiitic basalts and consist of subalkaline basalt and basaltic andesite as observed at Loukounga. These basalts are characterized by slightly low Nb concentrations (7 - 42 ppm) [51]. By comparison, the Loukounga lavas have Nb contents of between 4.64 and 28.4 ppm compatible with those of continental basalts of traps type (CFB). In the RD Congo, the equivalent of the Nemba complex, the Gangila basalts of the Zadinian Group are also described as traps basalts emplaced in the context of the rift [6].

In Brazil, the Araçuaï belt hanging from the Mayombe belt, carries neoproterozoic basalts of the Macaùbas and Dom Silvério emplaced in a continental rift context [52] or associated with arc context [32] [53] [54].

To determine the source of magma, the used TiO₂/Yb-Nb/Yb diagram of [55] shows concentration of Loukounga samples in E-MORB domain and some samples in OIB array (Figure 13(a)) and Th/Yb-Nb/Yb show concentration dispersed around E-MORB and volcanic arc array domains (Figure 13(b)). These fields proximity is characteristic of mantel crustal contamination [55]. The low Zr/Nb and high (La/Yb) ratios 3.67 - 6.77 of the Loukounga tholeiitic basalts (Table 1) characterize an enriched atmosphere and the Nb/Y ratio between 0.22 and 0.9 shows an addition from the melting of the mantle.

The Zr/Y-Nb/Y diagram of [56] modified [57] and Nb/Th-Zr /Nb diagram of [58] (Figure 14) characterize a metabasalt domain derived from an enriched mantle with dispersion in PM, REC, DEP, DM fields. The geochemistry variation observed in different magma with a mantle origin is due to continental crustal contamination or the Subcontinental lithosphere as suggested also [11] [14].