The Kenticha granite pegmatite field comprises monominiralic quartz, spodumene pegmatite, muscovite pegmatite, blocky microcline and muscovite-albite granite. The postorogenic granites are mainly composed of reddish and gray biotite granite and are high-K calcalkaline and highly siliceous. There are three different types of granites i.e., biotite granite, two mica granite and alaskitic granite. Their order of emplacement is biotite granite, two-mica granite, alaskitic granite, Albite + sericite + microcline + greisens + amazonite and finally pegmatites from older to younger. The alaskitic granites and the pegmatite bodies are injected as magmatic dikes into the host-rocks. This granite is characterized by lack of biotite, replacement of albite by K-feldspar and muscovite, and enrichment in quartz, Nb, Ta, Rb, Cs, Li and Sn and depleted in aluminium, titanium, magnesium, calcium, potassium, iron oxides, Sr, Ba, and Zr than the biotite and two-mica granites [26] [27] . It also shows alteration such as sericitization, albitization and kaolinization, and solution infiltration [27] .

Regional zoning of series of N-S trending barren to rare-metal enriched granite pegmatites in the area can be classified into five different types of pegmatites based on their geological and geochemical signatures [26] [29] [30] . These are (a) barren pegmatites, (b) Ta-poor pegmatites (Kilkele II and III, and Bupo II), (c) Ta-rich beryl-columbite subtype (Kilkele I and Dermidama), (d) complex spodumene type, and (e) albite spodumene type (Bupo I) (Figure 2). The regional zoning is also described in similar mineralogy, composition and texture with the above classification. Simple description as spodumene type for Kenticha rare metal pegmatite would not fit since it also consists of Li-silicates accommodated in lepidolite, spodumene, holmquistite, albite and swinfordite and Li-phosphates existed in the form of amblygonite and lithiophyllite [31] . Numerous veins and dikes in Kenticha show inward mineralogical and textural changes in an increasing in complexity parallel to the degree of pegmatite fractionation [29] . Such zoning and mineralogical changes from the rime to the core zones are caused by inward crystallization of hydrous magma [32] [33] . Consequently, inward changes in mineralogy is recognized from sodic aplite,

microcline-quartz-albite zone followed by quartz-muscovite-albite-spodumene zone to lenticular masses of greisen, lepidolite and quartz core units.

Different types of compositional zoning in Kenticha granite pegmatite such as oscillatory, patchy and mixed oscillatory has been identified [30] . The oscillatory zoning is developed as result of repetitive variations related to crystal growth processes, concentration of the major elements, segregation of gas-saturated magma and is consistent with the periodic variation in Ta, Nb, Mn and Fe contents. The texture of this zoning is manifested by relatively homogeneous core, zoned mantle and faceted border zone. The patchy zoning and other replacement textures of columbite-tantalite are formed by late-coming gaseous-rich chemical fluids resorption and replacement processes [30] . The late generation by replacement processes are relatively rich in Ta and Mn.

The Kenticha granites are compositionally peraluminous and fertile with varieties of minerals such as biotite, muscovite, tourmaline, spessartine, almandine, corderite and topaz. The Kenticha rare metal pegmatite belt comprises several groups of pegmatites which shows a fractionation trend. In situ fractionation of subhorizontal pegmatite sheet at Kenticha accounts for chemical and mineralogical zoning. The crystallization was occurred under closed system and contamination with the ultramafic host-rocks from the hangingwall was during postmagmatic hydrothermal stages [28] . Results of major and trace element analysis and their trends in ore, accessary and rock forming minerals suggest that these groups of granite-pegmatites are cogenetic in nature [26] .

The primary ore deposit (below 60 m depth) shows complex internal structure and variety of alternating paragenetic associations. The bottom of this ore body is muscovite and two-feldspar granite that grades upward into albite, muscovite-quartz-microcline and muscovite-quartz-albite-microcline pegmatite zones. The middle zone is dominated by muscovite-spodumene-microcline-albite pegmatite superimposed with albitized and greisenized linear units. The upper zone is the most differentiated pegmatite with spodumene, large quartz cores, microcline and ambigonite montebrasite blocks, and spodumene-quartz zones. The last stage of paragenesis dominated hydrothermally metasomatized mineral associations such as (a) fine to very fine grained and inequigranular tabular albites, (b) cleavalendite, (c) small flaky and coarse-flaky pink coloured Li-bearing muscovites, (d) lepidolite-quartz, and (e) quartz-albite and quartz-albite-muscovite associations [34] . Segregation of cleavalendite and lepidolite-qaurtz complex zones, and greizenized quartz cores and blocky microcline develop high amount of Ta contents in the metasomatically altered upper zones.

Similarly, the Ta content in the weathering mantle ore (above 60 m depth) is very high in metasomatic mineral associations and characterized by pronounced albitization and greisenization. While the low Ta content is found in ores associated with granite, muscovite-microcline-albite zones, and blocky microcline. The Ta content is also increased upward from bottom to top. Ta is associated with the columbite-tantalite group minerals forming flattened and short prismatic small grain crystals of 5 - 7 cm length [35] .

Uranium-lead age dating indicate that the emplacement of the Kenticha pegmatite was at ca. 530 Ma and temporally related to the post-collisional phase of granitic magmatism at 570 Ma - 520 Ma [41] . On the other hand the country/host-rocks are dated ~580 ± 50 Ma - 680 ± 30 Ma [30] . The emplacement of Kenticha and Bupo pegmatite is coeval and temporally related to postorogenic granite magmatism [10] [41] [42] . The intrusions of two-mica and alaskitic granites and the associated pegmatite swarms followed the regional fault system (Figure 7). The emplacement of pegmatites is controlled by folded and faulted structures trending N-S which could be related to the final stage of Katangan tectonogenesis [25] [43] . This forms the Kenticha Synclinal rare metal belt [26] . Thus, the evolution the Kenticha granite pegmatite start after the last tectonic stage of east African orogeny, i.e., post collision stage at ca. 620 Ma - 590 Ma [14] [44] [45] [46] .

The deep-seated faults are controlling the rare metal mineralization and the emplacement of the pegmatites (Figure 7(a)). Besides the deep-seated normal faults there are also minor normal faults that are trending NW-SE and NE-SW direction varying in their dip angle and direction. The orientation of the joint sets and the minor faults is similar which imply that the jointing was related with the minor faulting events. They all are striking NNW-SSE and NW-SE and dipping NNE and NE directions, respectively (see Figures 7(b)-(e)).

Numerous joints also observed in the area though currently they are obstructed by the mining activity. Tadesse (1998) grouped these joints into eight joint sets where their average strike varies from 30 to 60 relatively with higher dip amount and 170 to 277 relatively with lower dip amount [47] .

The Kenticha granite has been interpreted as Volcanic Arc Granite (VAG) and is related to subduction volcanism by Tadesse [29] . However, Mohammedyasin [36] interpreted as Within Plate Granite (WPG) to syn-Collisional Granite (syn-COLG) granite using whole rock geochemical analysis. Mohammedyasin [36] further proposed that the Kenticha granite pegmatite is probably sourced from (a) extreme fractionation of syn-to late tectonic granites (e.g., [33] ) or (b) anatexis process or in-situ partial melting of the metasedimentary rocks in the

area [48] [49] .

Among the various proposed models that explain the formation of pegmatites (a) the fractional crystallization of the melt and (a) interaction of aqueous fluid with the melt are the two competing models [50] . The concentration of fluxing components and other incompatible elements increase towards the centre of the magma chamber as crystallization proceeds resulting increasing chemical fractionation from the margin to the centre of the pegmatites [51] . The formation of giant crystals and exotic minerals however can be evidenced for the interaction of fluids and the melt by alkalis incongruent partitioning [52] such as the aqueous fluids enriched in K, and the melt enriched in Na. Later, the model of buoyant ascent, has been proposed by Jahns [53] in order to explain the chemical fractionation of the pegmatites.

Two end member models have been proposed for the formation of fertile pegmatites i.e., continuous crystallization and partial melting. Continuous crystallization of pre-existing parental rocks by partial melting which homogenize in a collective reservoir produces variety of granitic magmas depending on the degree of fractional crystallization. The varying degree of partial melting produces wide compositional variation of granite magmas. Partial melting of compositionally distinct protoliths can also produce wide compositional spectrum of granite magmas with the same degree of partial melting. This could be arise from the change mineralogy, trace element chemistry, mineral stability field of sheet silicates or accessory minerals and their content in the mineral/residuum phase, and metasomatic alteration of the source metasedimentary lithology [54] .

Partial melting of mica rich pre-existing metamorphic rocks in collisional zones commonly forms LCT granitic pegmatites and gives high concentration of trace and rare earth elements. Muscovite and biotite carry most of the trace elements. Abundant muscovite schist of marine sedimentary origin react extensively at the onset of anatexis [50] . Consequently, large fractions of the rare element content transferred to the initial small volume of partial melt. The melting reaction of muscovite and biotite also produce K-feldspar with some amount of alumunosilicate and spinel under low H₂O saturation condition (e.g., [55] ) of rubidium, slightly incompatible in K-feldspar. The ratio of Li and Cs, which are compatible elements in K-feldspar, is elevated as compared to Rb during consecutive crystallization resulting rare-alkali enrichment [56] .

The formation of rare-element granitic pegmatites is of mainly by fractional crystallization of a granitic melt [57] [58] [59] . Partial melting of appropriate composition (e.g., [54] ) such as metasedimentary Mn-bearing exhalites also proposed for the formation of these pegmatites [48] . From the tectonic setting, the Kenticha granite probably sourced from (a) extreme fractionation syn- to late tectonic granites (e.g., [33] ) or (b) anatexis process or in-situ partial melting of the metasedimentary rocks in the area [48] [49] . The genesis of the Kenticha pegmatite is similar with the Harney Peak and Tin Mountain granite pegmatites, Black Hills (South Dakota) and Ponta Negra, Brazil which is by partial melting of metasedimentary rocks with further strong fractional crystallization [32] [48] [54] . Besides, their tectonic setting is similar and related to post stage Gondwana assembly. Some of the data point also plotted in the limit and to the syn-collisional granite. This further indicates the formation of granite pegmatite can be also partly related to post-collisional processes during the post Gondwana assembly.

The relict textures in minerals such as relict of garnet in the studied samples can suggest for anatectic origin of granitic pegmatite [60] . The other evidence is the age of the Kenticha pegmatite (ca. 530 Ma; [41] ) which is bracketing with the time interval of Gondwana assembly and related to the collapse magmatism in the region (ca. 580 - 520 Ma; [61] ). Heilbron et al. [61] pointed out the heat that triggered this magmatic event could still be a consequence of the collisional orogeny. Küster et al. [41] also described that the Kenticha pegmatites are temporally related to the post-collisional phase of granitic magmatism (570 - 520 Ma). Uranium-Lead dating for the Kenticha tantalite in the spodumene zone gave an age of ca. 520 Ma. Based on age, the Kenticha pegmatite is formed after the cease of East African Orogeny (~550 Ma; [5] ). This further implies the origin of the granite and granite pegmatite is from an attenuated continental crust, not from an oceanic island granite [36] .

The increase in basal heat flow by ascending magmatic intrusion or collision causes partial melting of the pre-existing metasedimentary rocks. The later case is more reseanable for the Kenticha pegmatites since they are sturcurally located at a shear zone. During the ascent of the magma fractional crystalization and assimilation with the country rocks result different zonal mineral assemblages, geochemical variations and rare metal mineralizations (Figure 8). The ascent of the magma further could allow to melt the country rock which modify the composion of the magma. The incompatible elements such as Ta and Nb concequentely separate in the late stage of fractional crystalization. Fractionated compositions of pegmatite magmas and their final aqueous fluids are highly reactive with less-evolved to wall zone and host-rocks [62] [63] . Local contamination is occurred during the emplacement of the pegmatites along dike margins (metasomatic zone), and at the transition into sub-solidus conditions (Figure 8).

The parent rock for granites and pegmaite is probably the metasedimentary rocks which form felsic magma during the increase in temperature triggered by the collision orogeny.