The Mokama Cu bearing granite (DMMOKA-2-7 and DMMOKA-2-9) descriptions of gangue and ore minerals were performed under petrographic and metallographic microscopes, and Raman spectroscopy at Inha and Seoul National Universities, and results showed the occurrences of Cu mineralization as sulfides and oxide ore minerals (Figure 3, Figure 4). The mineralogical compositions of the Mokama granites consist of mainly silicates. This Mokama granite showed a phaneritic texture and consists of quartz, biotite, muscovite, k-feldspar (orthoclase), plagioclases, pyroxene and amphibole (hornblende), and accessory minerals such as zircon, ilmenite, fluorite, topaz, magnetite, and ore minerals including tin oxide group (TOG: Sn-W), columbite group minerals (CGM: Nb-Ta), and sulfide group minerals (SGM: Cu-Zn-Fe-As). Some granites showed relatively big-sized grains (>1 cm) of euhedral quartz and flakes of micas (abundant muscovite, rare biotite), and these grain sizes could display a lateral variation within the granitic body. Such rocks could be considered pegmatitic granites, they were rare and mineralized as well.

The Cu ore minerals (Table 1) consisted of essential chalcopyrite (CuFeS₂) that shows rims of chalcocite (Cu₂S), also lately replaced by covellite (CuS) and finally malachite (Cu₂CO₃(OH)₂) in the supergene zones (Figure 3(a), Figure 3(b), Figure 4(f)). The alteration that affected the KIB mineralized granites (especially in the mineralized Mokama granite, Figure 3(c)) consisted of quartz ± muscovite ± albite ( ± sericite) whereas the KIB barren granites showed quartz ± pyrite ± fluorite ( ± chlorite) (Figure 3(d)) or quartz ± albite ± chlorite. The presence and abundance of muscovite can be interpreted as an acidic environment where feldspars were transformed into muscovite (Figure 3(c)) [6] .

The barren granites (from the Barrage site, Figure 1) show abundant euhedral quartz grains and pinkish K-feldspar (orthoclase), while biotite, Fe-oxides, pyroxenes, and amphiboles are accessory minerals.

The Cu mineralization of the Mokama G4 granite in the Mesoproterozoic KIB is considered a late-stage magmatic-hydrothermal sulfide and disseminated

within the granitic rock compared to the sedimentary stratiform (and vein-type) Cu-Co of the Neoproterozoic Lufilian belt (LUB) in the great Katanga province In DRC [9] [13] [14] . In the KIB Mokama granites, the hypogene ore mineralization consisted of bornite, sphalerite, pyrite and chalcopyrite (Figures 4(a)-(e)). Bornite and chalcopyrite showed rims that are due to the later replacement by supergene sulfides such as chalcocite and covellite (Figures 4(a)-(c)), and these last ones were later on replaced by oxides such as the green mass of malachite (Figure 4(f)). Some sphalerite grains showed chalcopyrite diseases (Figure 4(d) & Figure 4(e)) and inclusions of silicate minerals (Figure 4(e)) that can be interpreted as associated with relatively high temperature-derived fluids. The occurrence of arsenopyrite is more likely associated with hydrothermal environment.

The Mokama G4 granites chemistry (XRF, LA-ICP-MS, Table 2) showed SiO₂ (71 wt% - 79 wt%), ASI (1.38 - 3.12 molar), and enriched in Rb (681 - 1000 ppm), Ta (12 - 151 ppm), Sn (43 - 142 ppm), Cu (10 - 4300 ppm), Zn (60 - 740 ppm), U (2.2 - 20.7 ppm) while depleted in Zr (20 –31 ppm), Sr (20 - 69 ppm), Hf (1.3 - 2.0 ppm), Th (2.2 - 18.9 ppm), W (9 - 113 ppm), Pb (5 - 50 ppm), Ge (5 - 10 ppm), Cs (21 - 53 ppm), and Bi (0.6 - 17.4 ppm). The Aluminum saturation index (ASI = 1.7 - 3.1) showed that this Mokama G4 granite can be considered a

peraluminous S-type leucogranites (Figures 5(a)-(c)), ferroan, highly potassic and calc-alkalitic. This Mokama granite is a late (post)-collisional granitoid, and is characterized by high Rb/Sr, Cu/As, Zn/As and (Ta/Zr)_N; and low (La/Yb) and Ba/Sr. This rock is also relatively enriched in Rb, Ta, Sn, Cu and REE (mostly HREE which are fractionated by pyroxenes and amphiboles). The ratios (La/Sm)_N, (La/Yb)_N, (Gd/Yb)_N, (Ta/Zr)_N and (Eu/Eu*)_N are 2.9 - 10.1, 0.1 - 11.5, 0.1 - 0.8, 113.3 - 2120.7, and 0.1 - 1.5 respectively.

The Kibara belt mineralized granites (granite s.s., pegmatite, peri-granitic quartz veins) in general and the Mokama granite in particular started by the precipitation of TOG, followed by CGM and ended with SGM of non-economic deposits.

(ID-inclusions), and CO₂-rich fluid inclusions (Figure 6(a) & Figure 6(b)). The microthermometric measurements (Linkam-FTIR 600, Inha University) were carried out essentially on fluid inclusions assemblages (FIAs) hosted in quartz, and consisted of liquid-rich and ID as of primary and pseudo-secondary fluid inclusions (Figure 6(a) & Figure 6(b)).

The results of fluid microthermometry can be used to determine the paleodepths and thermodynamic conditions (apparent salinity, homogenization temperature and pressure) of rocks and ore minerals as well [6] [16] . Microthermometric results (Table 3) of fluid inclusion assemblages (FIAs) hosted in quartz in the Mokama granite show ranges of salinities of 4 wt% - 23 wt% (NaCl equivalent)

and homogenization temperatures (Th) of 190˚C - 550˚C. A boiling assemblage in the granite suggests a fluid phase separation occurred at about 380 - 610 bars, and this corresponds to apparent paleodepths of approximately 1 - 2 km (lithostatic model) or 3 - 5 km (hydrostatic model). FIAs hosted in cassiterite (salinities of 2 wt% - 10 wt% and Th of 220˚C - 340˚C) set up the upper limit of SGM including Cu (-Fe-Zn-As) sulfides that probably precipitated at temperatures below 200˚C (Figure 7(a) & Figure 7(b)).

The Mokama G4 granites are peraluminous rocks associated with the Kibaran collisional event, and host huge critical and base metal potentials [10] [12] [18] . The magmatic-hydrothermal fluid processes that affected these granitic intrusions enable the mobility of elements and their precipitations inside and outside (country rock as hydrothermal veins) of the granitic intrusions. This is in consideration of many facts including the circulation of rising hot magmatic-hydrothermal reduced geofluids enriched in metal complexes (mostly chlorine and fluorine ligands, and rarely hydroxyl ligands), fluid-rock interactions with remobilization of metals from the host/country rock (lithologic control), mixing of fluids (hot saline magmatic-hydrothermal and cooler less saline meteoric waters) that possibly induced the oxidization, cooling-fugacity controls, and alteration that might be influenced and controlled the pH [6] .

Fluid inclusion data (quartz, cassiterite, fluorite) and the ore chemistry (oscillatory cassiterite, wolframite) showed that the TOGM (such as Sn-W) precipitated earlier, then followed by CGM (such as Nb, Ta, Li), and finally SGM (such

as Cu, Zn, As, Fe) that occurred at the very last stage. In the KIB, TOGM and CGM deposits are economically valuable whereas SGM is still now of non-economic value.

The KIB hosts Cu mineralization associated with magmatic-hydrothermal processes, and the LUB has Cu (Co) mineralization related to sedimentary (multi-source materials) processes. The Katanga supergroup relies directly on the KIB basement and has no compelled data and evidence that show the possible material connection between the two belts. Some researchers showed that the LUB sediments originated from many sources from Precambrian and Archean formations [7] [8] [9] [13] . A few questions remained unsolved especially when it comes to addressing the source of Cu and Cu mineralization. The occurrence of Cu mineralization in the KIB belt could possibly be the primary Cu feeder of the LUB by the remobilization of rising mineralizing fluids through the Katanga basin. The fact that the LUB is characterizable by Cu-Co deposits, makes the possibility of considering the KIB as Cu feeder very inconsistent and diminished. The best feeder of both Cu-Co metals would be intrusive mafic or ultramafic rocks; and in the nearby LUB area, such rocks have not been discovered or well documented. Another very unlikely source of LUB Co could be ultramafic dyke (peridotites) intrusions in the Archean Congo-Kasai craton that formed lately serpentinized bodies hosting Ni-Cr (with by Co-V-Zn as by products) in the regolith zones (such as in the Lutshatsha, Mfwamba, and Nkonko massifs) [19] . None of the above hypotheses or scenarios has been proven until today. Thus, despite some attempts to grasp the origin of Cu, the primary source of Co in the LUB remains totally unknown and requires more studies in the future.