The sulphide mineralization in the belt is not confined to a single lithology, instead it is a litho-package which is mineralized and this package is conspicuously calcareous in nature and is typically Marl. The principal facies of metamorphosed marl, hosting the sulphide mineralization are; Impure dolomite/marble, calcareous quartz biotite schist and to lesser extent calc silicate rock, besides

carbon phyllite which contains occasional layer parallel pyrite and pyrrhotite but no copper mineralization. The host lithlogy mentioned above have been discussed and the same has been mapped on large scale to elaborate on structures produced and their control on the mineralization, on map scale. (Figure 2(ii)).

The impure dolomite (includes amphibole bearing dolomite, biotite bearing dolomite and dolomite with intercalations of calc quartz biotite schist. And calc silicate (Figures 3(A)-(H)). Dolomite occurs as well bedded massive to semi massive, comparatively extensive subunit of the Ajabgarh Group of rocks in the

area. The average thickness of dolomite band varies from 30 m to more than 100 m at places. Characteristically the impurities in the dolomite, control the mineralization. The dolomite without impurities is typically barren. The abundance of amphibole bearing dolomite could be witnessed in the Baniwala ki Dhani block. On the other hand, the Dokan and Dokan North blocks have biotite bearing dolomite as the major mineralized lithology. Similarly, Dariba, Dariba north, Palaswala Ki Dhani and Toda Ramliyas blocks also have the dolomite as the predominant host but it is tremolite bearing marble here with partings of calc quartz biotite schist. Dolomite in the Toda Ramliyas, Palaswala Ki Dhani, Dariba and Dariba north blocks is also silicified in nature and traversed by subsequent quartz, carbonate, amphibole and chlorite veins, besides specularite veins. In the Dokan North block the dolomite is ferruginised in nature. Crystalline coarse grained variety of dolomite/dolomitic marble is also seen exposed in the Palaswala Ki Dhani and Dokan North block. This unit also exhibits occasional development of oxidised zones in terms of upper tough crust of ferruginous goethite material and very rarely crude psiolites of iron. Possible manganiferous coatings are also noticed on the surface of dolomite near Gursali ki Dhani village.

At few places the dolomite when becomes rich in tremolite, muscovite, and chlorite and assumes banded nature with bands of green minerals grading in to calc silicate rock, but it becomes difficult to separate these units, because of inter fingering nature of facies variation.

Calcareous Quartz biotite schist and biotite schist

Calcareous quartz biotite schist is another most prominent host lithology for copper mineralization, (has been referred as Calc QBS elsewhere) is exposed extensively as bedded lithology with well-developed schistosity. It generally exhibits spotted appearance at the expense of presence of coarse-grained plagioclase grains and also sometimes due to presence of scapolite. Rounded grains of calcite and quartz are also noticed as spots on the weathered surfaces. This unit seldom contains garnet porphyroblasts of varying dimensions. Frequency distribution as well as size of the scapolite porphyroblasts varies in large limits throughout the area. Scapolite defines a mineral lineation in Nanagwas and Dokan north blocks, while the smaller sized grains occur in the quartz biotite schist throughout the belt. The concentration of the calcite in this rock, after which it derives its calcareous nature, has large variation, it occurs as primary grains as well as secondary calcite as coating along the grain boundaries. The Calc QBS is so intricately intercalated with dolomite and biotite schist that it becomes very difficult some times to provide a nomenclature to the lithology, (Figure 3(D), Figure 3(E) and Figure 3(G), depicting various modes of occurrences and field expressions of Calc QBS)

Cal silicate rock

The calc silicate rock is well exposed on the eastern limb of the antiform in Dariba and Dariba north block; it is also well exposed in the Toda-Ramliyas block and in Palaswala ki Dhani block. This unit shows lateral facies variation from amphibole marble to calc-silicate rock. (Figure 3(H)). This mixed litho-unit has been termed as the inter-bedded calc silicate rock with calc quartz biotite schist. It is thinly bedded rock with greenish grey colour, having well defined scapolite rich bands and actinolite, epidote, calcite rich bands. The pink calcite veins emplaced parallel to these bands and litho-contacts are noted from this area. This unit is mineralized in Palaswala ki Dhani block where as it is barren in the northern parts of the belt.

Carbonaceous phyllite.

This litho unit occurs as intercalations within the Calc QBS and is rarely exposed on the surface. It is tuffaceous, very fine grained, soils the hand and ash grey in colour (Figure 3(F)) Very finely banded and thinly laminated. Generally, oxidised and contains non uniformly distributed red spots all over the rock surface, indicating presence of oxidised pyrite grains. In some of the areas like Dokan North block, Nanagwas block and Mahawa block this litho-unit contains a well-defined pyrite-pyrrhotite mineralized zone at a shallower level but does not contain any copper mineralization anywhere in the area in this zone. In some of the boreholes the carbon phyllite is intersected as sandwiched between quartzite and calc quartz biotite schist and contains graphitic development.

The general disposition of the litho-units in the area is North-North-East-South-South-West with steep to very steep dips on either side i.e. NW as well as NE direction. The rocks are intensely folded and preserve mesoscopic folds in calc silicate, Calc QBS, in dolomite and also in banded calc-semi-pelite litho-units besides the quartzite. Three principal planar surfaces are very well developed in the rocks of the area besides the bedding. The first foliation is parallel to the bedding and is comparatively less pervasive then the second. The S_ollS₁ has an acute inter-cleavage angle of about 15⁰ to 20⁰ with S₂ and both are steeply dipping. The direction of the dip keeps on swinging around the verticality. The third cleavage is widely spaced disjunctive in nature and least pervasive, does reflect refraction in various lithologies, and has nearly East-West trend. The area exposes and preserves three phases of folding very distinctly and profusely preserved on various scales.

The mesoscopic first folds; are, tight to isoclinal in geometry, (Figure 4(ii)) rootless, have various orientations indicating first deformation, and are recorded occasionally from the area. The first foliation is axial planar to the F₁ and is largely parallel to the bedding. Stripping lineation, mineral lineation defined by elliptical grains of scapolite, form the L₁ lineation. The F₁ folds can also be seen as intra-folial folds beautifully preserved in the Calc QBS and banded calc biotite schist. Stretched grains of sulphide and layer parallel mineralization recorded long the S₁, might suggest mineralization pre F₁ and alignment of the mineral bodies along s₁ during first deformation.

Second phase of folding: The Second fold is the most dominant structure in the area which controls the disposition of litho-units. It is preserved on macroscopic and mesoscopic scale in various lithologies. Mesoscopic F₂ folds are usually tight to isoclinal (Figure 4(i)) in nature. S₂ is represented as axial planar crenulation cleavage in mica schist and as disjunctive cleavage usually in the hinge part of F₂ folds in competent rock types. S₂ strikes N-S to NNE-SSW and is vertical to sub vertical towards west or west-northwest. The associated lineation (L₂) is recorded as intersection lineation (of S₀ and S₂), crenulation axis, minor congruous fold axis (S, Z, M-W folds, Figure 4(i)) and pucker axis. The lineation (L₂) pitches moderately towards S to SSW in the area. Displacement of S₀ is noted along the axial planar S₂ cleavage in competent rocks.

Macroscopic overturned F₂ folds are seen around Panchokharkhara, Patan, Mahawa, Bharala, Bageshwar, Baleshwar, Nanagwas, Dariba, Palaswala and Toda Ramliyas. In the Mahawa-Bharala-Bageshwar area, Mahawa synform is followed on the east by Bharala antiform, which is again followed by Bageshwar synform and thereafter by Dokan antiform (Figure 1(ii)). The second phase of folding has the major control over mineralization as the limb shears and axial planar shears parallel to the NNE–SSE trending axial planes are the prominent locales of the remobilized ore bodies. Besides the brittle ductile shearing, sympathetic to the D₂ deformation has also produced significant open spaces for the migration and deposition of the remobilized mineralizing fluids.

Third phase of folding: The third phase of folding in the area is marked by broad warps and open folds along nearly E-W striking axial plane and has also caused swinging of linear quartzite ridges. While this has not been seen on the surface but the curvilinear disposition of the ore lodes might suggest effect of the third phase of folding on mineralization.

Shearing: Evidences of shearing in NNE-SSW to N-S direction are profusely recorded in the area preferably in quartzite. The eastern and western contact of the Ajabgarh Group of rocks in the Valley with the Alwar Group of meta-sediments has a tectonised and sheared manifestation, evidenced by stretched pebbles of conglomerate, exposed West North West of Baleshwar temple, where the pebbles exhibit down dip lineation. Profuse silicification, epidotization, ferruginization and brecciation of the litho-units along the contact, and stretching of the grains and development of sigmoids and boudins in quartz veins support the tectonised nature of contact. A prominent brittle-ductile shear passing through the axial region of the antiform, which runs from Dariba to the Nanagwas block, here probably it enters subsurface and reappears in the Dokan-Baniwala and Dokan North block, displayed by brecciation, ferruginization and presence of tension gashes. Limb shears are also developed especially on the western limb of the Dariba antiform parallel to main shear plane. The bulk of the mineralization is also concentrated within these shear zones during deformation due to remobilization.

Faults: Major faults are not recorded from the area except for the ones reported earlier [3] in the Baleshwar area and the one reported [25] along the eastern limb of the Dokan antiform. East-West trending faults, north of Dariba and north of Gursali ki Dhani were recorded [36] . Besides this there are evidences of dragging along East-West direction in Bichhu Ki Dhani village, where drags could be observed in the carbon phyllite. Conjugate faults of mesoscopic nature have also been observed in Dariba, (Figure 4(iii)(B), and Figure 4(iii)(D)) Toda Ramliyas block and also at many other places, in the southern part of the studied area. In The Toda Ramliyas and Palaswala ki Dhani blocks conjugate set of faults disposed at an acute angle to the main fault plane which is East-West have been witnessed in the pits exhibiting slicken slides and indicating right lateral movement, are observed. The east west trending faults of the various intensities and dimensions are sympathetic and parallel to the axial planes of the third deformation. Some of these minor faults might have affected the ore body to go down on the eastern side is recorded during the drilling in Toda Ramliyas blocks and truncation of the lode in case of Southern extension of Nanagwas block.

The area forms part of the Alwar-Ajabgarh sub basin of the North Delhi Fold Belt and is important for hosting mineralization, dominantly base metals. Khetri Copper Belt is located west of the area and is separated by basement rocks. The area under study was known for Baleshwar copper deposit, which is the earliest mineralization known from this belt (Figure 5(i)). The principal minerals found in and around Baleshwar include Copper, Barite, Iron, Bismuth and REE, besides reported occurrences of gold and off course silver is associated with the copper. Calcite, feldspar and albitite veins are also reported from the area. The mining activity in this area probably dates back > 3000 B.C. as indicated by the

recent archaeological findings [1] . Considering the literary records, the mining is very well known from the Akbar’s period, since there is a mention of mining of Detha (Cobalt) from the Akwali Mine near Khetri, in Aiene Akbari, and the Baleshwar-Dariba is contemporary to Akwali. The Dariba village; 6 kilometres south from Baleshwar, is settled on the small mound of slag bears the testimony to the principal smelting site for ore from contemporary Baleshwar mine, besides having slag heaps at Baleshwar. The earliest geological record of the report of old working from the area is contained if references [20] [21] . Subsequently the exploration work by Geological Survey of India, from 1973-78, established mineralization to extend over a strike length of 1.5 km, as impersistant lenses and 1.59 million tones of reserves were estimated, at 0.84% Cu at 0.50% Cu, cut off [3] . Old workings for barite which is hosted within the impure marble and calc silicate rock and controlled by the F₂ deformation, is exhausted now; is located at Sami ki Dhani area and is known as Kharagbinjpur Barite deposit [37] . Calcite, Iron and feldspar are also mined from the Raipur area, near Nanagwas [37] . The iron deposit is located south East of the Baleshwar and nearly 4 km south west of Raipur, which is 10 m - 50 m wide and nearly 500 m in strike length, has a very high content of magnetite with some hematite. Significant hematite quartzite bands are also reported from the area under study in the Toda-Dipas transect, having an exposed width of about 35 m and strike extension of about 2 km each of these en’echelon disposed bands, [38] [39] . Bismuth ore occurs in Narda [40] in earthy and lumpy form as segregation, within pegmatite with values of the order of 2% to 4% Bi. The Bismuth values from 50 ppm to 3000 ppm occur in a variety of rock types including pegmatite and albitite around Narda hill and in the adjacent Nim-Ka-Thana area. The study of bismuth in this area assumes more significance since upto 7000 ppb Au and 1000 ppm Ag have been recorded from the ore. Albitite and magnetite veins are also reported from the Narda area besides Native Gold and Bismuth. Drilling carried out for Bismuth in the same area however could not prove any resource [41] . The surface geochemical mapping by GSI, established a prominent zinc anomaly in the area, South East of Kharagbinjpur and few boreholes were drilled [42] [43] [44] . Occurrence of Gold and REE mineralization has been reported in EPMA studies from the Toda Ramliyas block [33] . Despite the area having 2000 year old mining history and the copper mineralization being worked out in detail by GSI, during late seventies at Baleshwar, the bornite dominated copper mineralization hosted within the impure dolomite and calc silicate, occurring as disseminated and fracture filled mineralization remained un discovered till the year 2000. Ever since this mineralization has been unraveled it is being explored continuously till date by Geological Survey of India, Jaipur, of which the present author was part of, along with other workers whose works are reported here. Which has augmented the national copper resources significantly and the area has emerged as one of the important copper silver mineralized belt, on Mineral map of Rajasthan.

The mineralized zone/sulphide zones as studied from the borehole cores and surface are characterized by presence of disseminations of bornite, chalcopyrite, covellite and chalcocite. Occasional clusters of the coarse grained bornite within quartz, carbonate, chlorite and amphibole veins are noticed besides the stringers of various sulphides. Occurrence of small sigmoid and lenticular bodies of quartz and carbonate, containing disseminations of sulphides and aligned parallel to the banding in the marble and along the foliation in the calc-quartz biotite schist, (S_oIIS₁), have been observed in various borehole drill cores throughout the area. The fracture filled and vein filled sulphides within the quartz and calcite veins are recorded in considerable proportion from the area. Very fine grained dusty disseminations of bornite and sometimes chalcopyrite are also recorded specifically from the biotite bearing rocks. Pyrite in general occurs as poor disseminations all along the drilled depths of various boreholes. Occasional pyrite veins are also recorded. A well defined layer parallel pyrite mineralized zone occurs at shallow level in almost all the boreholes drilled in Dokan and Dokan north blocks. Specular hematite occurs as vein filling, fracture filling cutting across the foliations besides wide spread disseminations in various rocks all through the area. Galena associated with the pyrite and specularite occurs in Nanagwas block and random veins in other places. Covellite occurs as vein fillings and as coatings along the pyrite and bornite besides streaks and stringers. Foliation parallel bornite streaks and stringers are frequently observed. Pyrrhotite also occurs as wide spread mineral and very often associated with the bornite. The co-existence of bornite and chalcopyrite is not always seen but very often they occur together. Larger chunks of coarse grained bornite and pyrrhotite occurring together have been observed. In Mahawa block the shallower level mineralized zone is richer in bornite while the deeper level (comparatively; otherwise both the zones are within 100 m depth from the surface) contains more of chalcopyrite than bornite. Such variations and aberrations to generalization are noticed throughout the belt in various blocks but the general mode of occurrences include, disseminations, streaks, stringers, vug filling, cavity filling, layer parallel and co-folded pyrite and pyrrhotite veins (Figure 6 & Figure 7). The presence of vein fillings of bornite-chalcopyrite, covellite, and chalcocite suggest remobilized and epigenetic component of mineralization. Occurrence of smears of bornite, (Figure 6(A)) chalcopyrite, pyrite and other sulphides suggest circulation of mineralizing fluids along the fracture planes.

The mineralization in the area is characterized by over lapping signatures of litho and structural control. The mineralization primarily is hosted within the

calcareous facies by and large. The impurities in marble/dolomite are in terms of varied proportion of biotite, amphibole and calc silicate minerals. Another litho-unit containing the mineralization is calc-quartz-biotite schist and/or calcbiotite amphibole schist with or without garnet and scapolite. Occurrence of wide spread, dusty and impregnated disseminations of bornite, chalcopyrite, covellite and specular hematite within various calcareous rocks, layer parallel pyrite and pyrrhotite mineralization, sulphide veins co-folded with the host lithology (observed in drill cores in Mahawa area) suggest the nature of primary mineralization to be of syngenetic in origin, as one of the modes of mineralization in the area. However, the significant proportion of the mineralization is observed as coarse grained aggregates and chunks associated with quartz and calcite veins. These veins are emplaced oblique to the banding, indicating the epigenetic/remobilized component of mineralization. The occurrence of coarse grained bornite and chalcopyrite in these veins suggest recrystallization. Besides the occurrence of mineralization associated with the calcareous rocks, carbonaceous phyllite and phyllite also found to be containing some layer parallel pyrite and pyrrhotite mineralization.

The mineralization is mostly associated with the hybrid type of rocks i.e. scapolite bearing amphibole marble intercalated with dolomitic marble, dolomitic marble with biotite partings, calc quartz biotite schist, calc quartz biotite schist with partings of amphibole marble and scapolite bearing amphibole marble with calc quartz biotite schist and calc silicate partings. This mixed kind of litho-package suggests that the mineralization is preferably localized along the zones of depositional facies variation. The sulphides were precipitated during the deposition of lithofacies. The coarsely crystalline nature of the sulphides and their association with amphibole, quartz and calcite veins indicate that a part of the mineralization is remobilized and relocated along the weak planes during the post depositional diagenetic/metamorphic and/or deformational activities. Occurrence of zeodes of quartz, associated with the mineralization, suggests hydrothermal epigenetic origin of the sulphide mineralization. Yet another feature observed from the drill cores, i.e. occurrence of foliation parallel stringers and veins of the sulphide co folded with the foliation suggests its origin to be syn to pre F₂ or D₂ deformation, in this area.

The restricted occurrence of silver in the Dokan, Baniwala ki Dhani and Kundla ki Dhani blocks, which are on the northern end of the belt and in the Toda Ramliyas block on the southern end of the mineralized belt and conspicuous absence of silver from the central and middle part of the belt, might indicate a typical basin configuration. It is known that silver goes preferably in to the lattice of chalcocite by its geochemical affinity, as chalcocite forms the earliest mineral in a sedimentary basin grading from deeper parts through chalcocite-bornite chalcopyrite-pyrite-pyrrhotite and hematite in the last, towards the outer shallower parts of the basin. These blocks namely Baniwala ki Dhani, Dokan, Kundla ki Dhani in the north and Toda Ramliyas block in the southern end contain considerable amount of chalcocite meaning there by the Dokan and Baniwala ki Dhani and Kundla ki Dhani was the deepest part of the basin during the time of deposition, hence it is restricted to these three blocks. Similarly silver association is repeated in the Toda Ramliyas area which is the southernmost part of the Dokan-Dariba mineralized belt, where hypogene environment of mineralization has been suggested [16] . The enrichment in Chalcocite and occurrence of hematite bornite ex-solution in this area along with silver association suggest occurrence of a horse shoe type of structure where the southern and northern parts of the areas indicate deeper part of the basin having richer mineralization while the middle part/central part of the area is shallower part, where the mineralization is weaker. The mineralization beyond Toda Ramliyas is not seen in south, which appears to be truncated by the profuse pegmatite intrusion which has eaten away the already weak mineralization. These Pegmatites and Granites possibly have facilitated the induction of hypogene environment.

Hence the mineralization here in this entire area is syn sedimentary, which was remobilized and scavenged and relocated within the structurally favourable locales like brittle shear zones by the mineralizing fluids during the deformation. The epigenetic hydrothermal component of mineralization is represented by mineralized veins disposed oblique to the lithology and might have its source in the hydrothermal fluids derived from the granitic and pegmatite plutons present in the area, which is substantiated by EPMA studies also. The absence of deformation textures in ore minerals might point towards the syn to post D₂ deformation emplacement of the epigenetic component of the mineralization. The preferential occurrence of mineralized zones within the brittle ductile shear zones, which are sympathetic to the main NNE-SSW shear zone, disposed parallel to the axial zone of the major F₂ folds in the area, suggest structural control on mineralization. Hence the sulphide mineralization in the area is primarily lithologically controlled and has been re-concentrated in the present locales, during metamorphism and/or deformation and these mineralized zones are thin, parallel and disposed in en-echelon pattern within the axial zone to western limb of the major F₂ structures in the area.

It has been observed that the mineralization in this belt is confined to the marly package, and by very nature of environment of deposition the marly package has facies variation, accordingly the host lithologies are also exhibiting a mixed kind of mineral composition of the rocks exposed in the area. These litho units include dolomite which has graded to marble at some places and is characterized by varying proportions of various impurities, which leads to the facies as Tremolite bearing dolomite/marble, Amphibole bearing marble/dolomite, Biotite bearing Marble/dolomite and siliceous dolomite/marble. Similarly other predominant lithology, which is largely mineralized across all the blocks is the calcareous quartz biotite schist, which has been referred as calc QBS in the text at many places. This QBS occurs with or without scapolite, and garnet. The thin laminas like partings of calcareous quartz biotite schist occur within dolomite. As one moves southward in this belt the calc silicate rock is also mineralized, where as in the blocks falling in the north within the mineralized belt calc silicate is almost barren.

The petrographic studies of a large number of thin sections of the various lithology intersected in boreholes, as well as from the surface has been done, here in the following section a summarized account of the observations and representative photomicrographs have been presented to represent the petrographic characteristics of the host lithology and their relation with the mineralization. It is recorded that there is a predominance of minerals like biotite, chlorite, actinolite and tremolite indicating upper green schist facies of metamorphism in general but isolated occurrence of garnet and hornblende in some cases indicates that the metamorphism touched the pressure temperature conditions of amphibolite faces, though not as uniform and wide spread. The host rocks are, coarse to medium grained in nature, and the sizeable portion of the rock, sometimes is purely composed of calcite and actinolite indicating profuse carbonate and amphibole venation in the area. The important lithology with reference to mineralization is marble/dolomite which contains nearly 10% to 15% and even more biotite, (Figures 8(A)-(F)) actinolite and tremolite (in various different localities) along with minor chlorite. Scapolite occurs associated with biotite rich marble bands (Figure 8(E)). The actinolite clusters are very common in the marble (Figure 8(D)). Secondary calcite in the form of veins and coarsely crystalline aggregate are also observed (Figure 8(A)). The feldspar, primarily the potash feldspar, mostly orthoclase depicting sericitization and containing profuse inclusions of quartz has been observed very commonly (Figure 8(D)). The principal minerals which occur in the quartz-biotite schist are quartz-biotite and feldspar (potash feldspar mostly orthoclase) and sub ordinate plagioclase of calcic type. The biotite occurs as primary grains showing preferred orientation and imparts schistosity to the rock (Figures 9(A)-(G)). The schistosity is generally poor except for the portions richer in biotite displaying well developed schistosity. Secondary biotite mostly occurs as cloudy grains, masking other optical features and lying oblique to the principal foliation, is observed (Figure 8(F)). The characteristics of various minerals which are often psedumorphed by sulphides are depicted in Figures 9(A)-(F) and Figures 10(A)-(F). Quartz which is the next most important mineral occurs as equigranular to irregular in shape and displays saccrohidal texture and wavy extinction. Tourmaline occurs as accessory mineral with rounded to stub like porphyroblasts, irregularly distributed throughout the rock mass. Garnet and Scapolite also recorded from the Calc-QBS, having a large size range (Figure 9(G) & Figure 9(A)). Occurrence of preferred alignment of prismatic grains of opaques indicates syngenetic type of mineralization (Figure 9(D) & Figure 10(C)).

The opaques occupying the cleavage planes of hornblende and alignment of

the same along both the schistosity and vein fillings of sulphides healing the weak planes are suggestive of the epigenetic nature of mineralization (Figure 10(A) & Figure 10(E)). Occurrence of crenulation cleavage has been observed in micaceous rocks, in some of the cases the crenulation axis is very well demarcated by the crystallization of epidote, sericite and garnet along it (Figure 10(F)). Minute plagioclase grains are also noted from this litho unit. The calc silicate rock becomes important as it is mineralized in Toda Ramliyas and its northern extension blocks. This is coarse grained rock with well developed schistosity. The mineralization is mostly in the form of vein filling, with occasional clusters of sulphides. A litho unit similar to the calc silicate rock has been recorded from the Baniwala ki Dhani block which is a calcareous rock but at places contains nearly 10% to 20% amphibole and has been marked as amphibole marble is mineralized profusely in Baniwala ki Dhani block [48] . Besides amphibole the rock contains scapolite and other calc silicate minerals, plagioclase and secondary calcite. Such rock has not been repeated anywhere in the belt. The characteristics of calc silicate rock are depicted in Figure 9(A), Figure 9(C) & Figure 9(F).

Exhaustive petrography of the host rock as well as the ore lumps has been done in the entire belt under various blocks; the nature of mineralization as exhibited by ore petrography indicates nearly similar textures throughout the belt except some variations in the southern sector. Here a summarized account of the vast amount of observations made has been presented, taking all salient features from various blocks, to make the study and behaviour of the mineralizing fluids representative of the mineralized belt.

The ore petrography study depicts occurrence of bornite, chalcocite, diginite, covellite, chalcopyrite, cubanite, pyrrhotite, pyrite and specular-hematite, magnetite, besides the occasional grains of galena. The Allanite has also been reported from the area. The bornite occurs mostly in the form of large coarse grains with irregular boundaries in association with other sulphides, occurring as islands within the chalcopyrite and vice versa, suggesting reverse paragenesis (Figure 11(ii)(A), & Figure 11(ii)(C)). The normal and reverse paragenesis is evident in the area suggesting towards the disruption of paragenesis during the post depositional remobilization of the ore fluids. It also occurs as bold grains adjacent to pyrite indicting eutectic crystallization (Figure 11(ii)(B)). Bornite has also been recorded being traversed by the veins of other minerals like chalcopyrite (Figure 11(ii)(A). Bornite occurs in exsolution and intergrowth with chalcopyrite, (Figure 11(i)(F)) covellite, chalcocite and specular hematite. The intergrowth with hematite (Figure 11(i)(C)) suggests presence of hypogene environment of ore formation. The covellite by and large occurs mostly as alteration product,

preferably confined to the cleavage plains of bornite (Figure 11(ii)(D), but incidences of independent grains of covellite have also been noted (Figure 11(i)(F). Chalcocite and covellite in some cases occur side by side as simultaneously crystallized grains. Pyrite and pyrrhotite showing normal and reverse paragenesis with bornite are observed, as islands of bornite within chalcopyrite and pyrite and islands of pyrrhotite and pyrite within large crystals of bornite are observed (Figure 11(i)(A) and Figure 11(ii)(C). In general the bornite grains are coarse and have irregular and straight grain boundaries with the other associated minerals. This indicates simultaneous crystallization, but veins of pyrite as well as that of bornite cross cutting each other are also observed. Chalcopyrite is also significant mineral which is associated with the other sulphides, though the relative abundance is less than bornite. Chalcopyrite grains generally become significant, when they are bold large porphyroblasts sharing straight grain boundaries with other sulphides and occur as fracture fillings. Besides this commonest mode of occurrences, the fine disseminations, stringers and streaks of the chalcopyritebornite are common mode of occurrence.

Remobilization evidences are beautifully depicted by hair thin veins of chalcopyrite originating from a larger grain and cutting across various other sulphide and gangue. (Figure 11(ii)) Healing of fractures in gangues and within the other sulphide minerals are also some of the abundant mode of disposition of the chalcopyrite ore bodies. Typical replacement textures depicting chalcopyrite altering to covellite to chalcocite is observed from the area (Figure 11(i)(E)) features like exsolution, and various replacements of minerals by each other are depicted in Figures 11-15. The effect of post depositional deformation is preserved in the form of fractures and occasional granulation of above all ore minerals. Most commonly exhibited texture is the cataclastic grains of pyrite and pyrrhotite (Figures 16(B)-(D)). Some deformed grains of pyrite and chalcopyrite have also been observed; never the less, evidences of significant post depositional deformation of ore are seen restricted to the above observations, in the entire belt. The predominant gangue minerals are biotite, epidote, hornblende, tremolite, actinolite, quartz, calcite and scapolite. Occurrence of short prismatic grains of pyrite and pyrrhotite aligned parallel to the foliation in the rocks of the area does point towards the syngeneic nature of the mineralization. Similar features have also been observed in the borehole cores in hand specimens, where the layered pyrite and pyrrhotite is co-folded with the foliation suggesting the syngeneic nature of mineralization. Contrary to that there are several incidences of the mineralization being in the form of fracture filling and vein filling cutting across the foliation indicating towards the epigenetic and or diagenetic nature of the mineralization in the area. Hence the area hosts the evidences of both the syngenetic as well as the epigenetic and diagenetic nature of mineralization. Most common textures observed are the intergrowth, exsolution and replacements.

Besides the above summarized and generalized characters of the ore under microscope from the belt, there are salient observations made regarding the variation in the behaviour of the ore minerals from north to south in the belt, which merit a mention here and can lead to significant contribution in the modeling for the genesis and localization of mineralization in the belt.

1) The predominant sulphide minerals found in the area and recorded during the ore petrography are; pyrite-pyrrhotite-bornite-diginite-chalcopyrite-covellitechalcocite with occasional presence of galena. Hematite as prominent oxide phase with magnetite and Ilmenite.

2) The predominance of bornite over other sulphides, remains a common feature throughout the area, but within this setup there are certain variations, for example in Mahawa area/block the bornite and chalcopyrite are found in separate zones indicating a possible mineral zoning. The proportion of bornite is maximum once again in Baniwala ki Dhani-Dokan blocks, it still maintains pre-dominant in other blocks located within Dariba antiform and Dokan antiform but the proportion of chalcocite gains significance as one moves from north to south in the area, i.e. South of Dariba antiform. The chalcocite is predominant over bornite and chalocopyrite in the Toda Ramliyas and its adjacent blocks, while it is insignificant in Palaswala ki Dhani block, where chalcopyrite is the main ore mineral.

3) The occurrence of Galena in the form of Lead lode is restricted to the West of Nanagwas block, while lead values have also been recorded from Mahawa block and myrmekitic galena from Nathuwala area.

4) The association of silver is restricted to the Baniwala Ki Dhani [47] Dokan blocks only as Cu-Ag lodes, [48] while stray incidences of silver are also reported from the Panchokharkhara [49] [50] and Toda Ramliyas (N) blocks [51] .

5) The occurrence of hematite as impregnated disseminations of prismatic grains in groundmass in the host rock have been seen throughout the area, but from the Dariba block further south the intergrowth of Hematite and Bornite

has become more significant. The intergrowth of hematite and bornite, predominance of chalcocite and occurrence of silver supported by presence of REE bearing minerals xenotime and allanite from southern sectors of the belt together suggest the establishment of hypogene environment of ore formation in this part during the emplacement of Plutons (Granites and pegmatites) syn to post D₂ deformation [16] .

6) Though the plutonic intrusive activity is responsible for partial enrichment of the mineralization with depth in the southern most sector (observed in Toda Ramliyas block) of the belt, reflected in terms of marginally higher grade of Cu, yet the same intrusive phase is also responsible for termination of the mineralization further south, where it has disrupted the host litho-package and totally eaten out the mineralization at the expense of profuse pegmatite emplacement.

The electron probe micro analysis studies of the ore sections from the belt have been carried out on CAMECA-SX-51 & CAMECA-SX-100 instrument at Geological Survey of India EPMA Lab Faridabad and Kolkata, over a period of two decades under different blocks and projects, here in the present paper only representative data has been presented. The EPMA results of Northern part of the belt including the Dokan Block, Baniwala-Kundla ki Dhani and that of west of Nanagwas Block have been discussed here. The studies have been carried out in Dariba and southern extension of Nanagwas Block also but that data does not show significant genetic signatures of sulphide or association of depositional environment indicator minerals. The southern sector encompassing Toda Ramliyas block and Northern extension of the same has some significant indications; these have been discussed here to arrive comprehensively at some genetic model. The analytical studies are carried out on the polished ore surfaces from Dokan, Kundla Ki Dhani and Dokan North blocks suggest large variation in the physicochemical conditions of crystallization of copper and silver associated with other sulphides. The detailed elemental composition of various sulphide ores are depicted in the Tables 2-5. The temperature of the minerals recorded in the electron probe studies indicate, derivation of some minerals from pegmatite on one hand, while other minerals suggest a normal epigenetic hydrothermal depositional

environment. Some of the sulphide minerals are observed to occupy the lattice of the bornite at high temperature besides silver. These minerals having minor occurrences mostly occur as exsolution, hydrothermal veins and vermicular wisps in the bornite. Silver is most commonly associated with the chalcocite, (Figure 17) occurs as native grains but also found to be associated with many sulphides including wittichenite, parkerite, aguilarite and carrollite (Figure 18).

The electron probe studies from the area have recorded some of the sulphide minerals for the first time, besides, identifying various associations of known minerals. The sulphides include bornite, chalcopyrite, chalcocite, covellite, galena, parkerite, wittichenite, carrollite, aguilarite, enargite and argentite besides, Ag-Cu sulphides, Ag-Cu-Bi sulphides and Ag-Cu-Fe sulphides (Figure 18). The above associations of sulphides and silver call for the existence of many geochemical systems operating together during the process of sulphides precipitation and emplacement in this belt. The geochemical systems operating during the process are Copper-Sulphur system, which has produced principally covellite and chalcocite. Another important system is Copper-Iron-Sulphur system producing the Bornite-Chalcopyrite-Pyrite minerals. These are the crystallization systems which have controlled the bulk of the sulphide mineralization in the belt, but there are small and less common but important geochemical systems operated in various parts of the belt are Nickel-Bismuth-Sulphur system, Cobalt-Nickel-Silver system, Copper-Bismuth-Silver system, Copper-Cobalt-Sulphur system, besides, native silver has also been found in the probe (Figure 18 & Figure 19). It could be observed with confidence that besides the above mentioned various geochemical systems, there has been large scale substitution of various elements in different proportions which has allowed the crystallization of various

minerals, which are not generally in equilibrium with the common systems controlling the bulk of the mineralization. The common solid solutions and intermediate solid solutions (iss) allow a limited substitution of the element in equilibrium at various temperatures as in a copper-iron system, only 3 atom % of copper in pyrrhotite is permitted at 700˚C [54] [55] , similarly the highest content of copper in pyrite can occur at lower temperature than at higher temperature [56] . The presence of Zn in Copper-Iron-Sulphur system can significantly alter the phase relations at high temperature, but at low temperature zinc will exsolve as sphalerite. The solid solution with ZnS, so stabilizes the iss that chalcopyrite becomes incompatible with the sphalerite just below 500˚C [57] . The geochemical system Copper-Iron-Nickel-Sulphur is very important for the magmatic segregation deposits, but not so important for the hydrothermal deposits, occurrence of copper, nickel, cobalt and sulphides of selenium in combination with copper and silver suggest the presence of either hydrothermal or high temperature metamorphic environment of formation of such minerals. The silver is hosted in pentlandite due to stability of its structure having the composition Iron-Nickel-Silver sulphide and Argentinean pentlandite is the principal host of silver in many magmatic deposits [58] . But, in the present case the silver metal is exsolved from bornite and occurs in the various combinations of copper sulphur system of crystallization suggests that the bulk of the present mineralization is not a magmatic segregation deposit. However, the occurrences of other minerals like Wittichenite which crystallizes at 527˚C (high variety) and 290˚C (low variety) in the form of hydrothermal veins in association with other Bismuth minerals. Aguilarite, Argentite, Parkerite and Carrollite do indicate the presence of hydrothermal environment of deposition having a varied temperature range. Carrollite crystallizes in Copper-Cobalt-Sulphur system and is found to occur in association with chalcocite, covellite, bornite, tetrahedrite, chalcopyrite and digenite, besides pyrite, sphalerite and calcite. It has been found that carrollite co-exists with chalcocite at 500˚C and is more copper rich. Parkerite mostly found in Nickel-Bismuth-Sulphide system associated to pegmatite or marginally magmatic nickel ferrous Pyrrhotite, where it is associated with the pentlandite, chalcopyrite, cubanite and galena and bismuth telluride. Argentite occurs as epigenetic veins near surface in association with galena, sphalerite, pyrite, chalcopyrite and native silver in hypogene process. Aguilarite, predominantly silver selenium sulphides with minor Cu and Pb are low temperature hydrothermal mineral and occurs associated with the copper-sulphur geochemical system indicates the substitution of Ag by Cu as well as by Pb in a hydrothermal environment. The principal combinations and associations of mineral phases in the northern sector, based on petrography and electron probe study combined can be summed up as:

Parkerite and Carrollite, Aguilarite, Wittichenite, Argentite and other minerals could only be identified as blebs and fresh fills within the bornite and as thin hydrothermal veins traversing the bornite porphyroblasts so also native silver shows exsolved nature from bornite and chalcocite by electron probe. Besides these sulphides, oxides like Magnetite and Specular Haematite also have been observed from the area. These occur as intergrowths with bornite.

The electron probe analysis of the samples from the West of Nanagwas block indicates peculiar and uncommon intergrowth of sulphide and oxide where a bornite grain contains a lath of a euhedral shaped specularite (Hematite) (Figure 19(B)). Similar intergrowth has been noticed from the Dariba and Toda Ramliyas block even under ore petrography. This intergrowth may be attributed to hypogene formation in an oxidizing environment [57] Hematite, ilmenite (Figure 15(B)), a native bismuth grain has also been observed in the BSE images of a sample from the southern part of the block. The association of ilemenite is significant as it is a geologic thermometer and indicates the deposit touched at least 500˚C temperature during its formation [57] . The geochemical systems operating during the process are Copper-Sulphur system, which has produced principally covellite and chalcocite, another important system is Copper-Iron-Sulphur system producing the Bornite-Chalcopyrite-Pyrite minerals. It is observed that the bornite of Dokan block appears enriched in iron which ranges between 10.1% to 11.1%, in comparison to bornite analysis from Nanagwas block, which has a larger range from 5.30% to 11.5%. Titanium association with bornite is reported from Nanagwas area [60] [61] . The points with high bismuth values show anomalous values of tin also.

The EPMA study of sulphides from Dariba north which forms part of the Central sector located within the main antiform structure; the Dariba antiform indicates that sulphides are present in the form of fine to very fine disseminations. The ore minerals such as chalcopyrite, chalcocite and bornite occur as fine disseminations and at most of the sections studied indicate chalcocite, bornite replacement [62] . The rhombic, cubic shaped pyrite shows sieved texture. Sphalerite and galena show close association with the chalcopyrite. Thin slender grains of magnetite occur as discrete grains within the matrix of biotite.

The electron probe analysis of the samples from the southern sector; Toda Ramliyas block and its extension comprising the southern sector of the belt, have been carried out for selected core samples collected from different depths. The elements analyzed are Fe, Co, Cu, Zn, Ag, Bi, Au and S. The copper mineralization in Toda-Ramliyas block [33] occurs not only in the form of fine disseminations of Chalcocite, Bornite, Chalcopyrite and occasional Chalcocite but also along the secondary quartz & calcite vein. The samples show replacement texture exhibiting replacement of bornite by chalcocite (Figure 20). A good association of chalcocite and bornite has been noted almost in all samples. One yttrium (Y)-bearing phosphate phase (Xenotime) has been identified in one sample in association with chalcocite and bornite. Xenotime is a rare-earth phosphate mineral, the major component of which is yttrium ortho-phosphate (YPO₄). Fine disseminated magnetite also identified along with the other sulphide minerals. Intergrowth of sulphide and oxide has been observed, here also like Nanagwas and Dariba (Bornite-Hematite intergrowth).This intergrowth may be attributed to hypogene formation in an oxidizing environment [57] . A very good intergrowth texture of bornite and chalcocite has also been identified in a sample. Besides magnetite, ilmenite, native silver (Ag), Grains of galena (PBS) have been noticed in the samples, Bismuth (Bi) phase also identified An allanite grain in BSE image and by wavelength-dispersive-spectrometry (WDS) has been identified in (Figures 20(A)-(D)). Allanite is a sorosilicate group of minerals within the broader epidote group that contains a significant amount of rare-earth elements. The above associations of sulphides indicate the existence of more than one geochemical systems operating together during the process of sulphides precipitation/emplacement. The chalcocite occurs here in two different modes; one as alteration product of bornite and second as independent bold

grains occurring separately. Such independent grains might suggest hypogene origin of chalcocite apart from chalcocite as alteration product of bornite.

The various geochemical systems discussed and mentioned above have their specific temperature stability range and these stability fields of various minerals decide the exsolution and iss. Here the mineral having the largest stability range in terms of temperature is bornite as well as pyrrhotite. Besides this Ilmenite also determines the temperature range as it is completely miscible with hematite above 600˚C temperature while separates out at 500˚C, [57] . The pyrrhotite and pyrite are inter-convertible at various temperatures; hence they occur associated to bornite and chalcopyrite both and do not actually signify any particular temperature range for the deposit where they are occurring. But the occurrence of Aguilarite, defines the lower temperature range at 133˚C, while the upper range as indicated by the presence of wittichenite, which requires a temperature of about 570˚C. Hence, the sulphide mineralization has been deposited between 133˚C and 570˚C temperature, as deduced from the electron probe studies of sulphides from the belt.

Fluid inclusion studies can define the temperature and pressure conditions of the emplacement of ore fluids besides indicating the nature of the fluid which helps indirectly to infer as what could have been the source of the fluids causing mineralization. Such studies have been carried out in various blocks of the mineralized belt. The significant observations have only been made in two blocks namely Baniwala ki Dhani block which could be taken as representative for the other three blocks including the Dokan north block, Dokan block and Kundla ki Dhani block, because the nature of mineralization, correlation of sulphide zones as well as copper lode is achieved with the high degree of similarity in these four blocks. Another significant block where fluid inclusion studies have been carried out is the West of Nanagwas block which is confined to an independent mesoscopic structure and mineralized lodes do not lie in the exact strike continuity of the other four blocks has been discussed here. However it forms part of the Northern sector.

Fluid Inclusion studies have been carried out in Central Petrological laboratories, Geological Survey of India, Kolkata using Leica DMLP (TMS 94), GSI for micro thermometry studies of samples and temperature was controlled with the Linksys software.

Total 22 samples were collected both from mineralized and non-mineralized part of cores of different boreholes of West of Nanagwas area. Thin wafers were prepared at Petrological lab, WR, Jaipur. 22 samples have been studied and out of 22 samples workable inclusions have been found only in 4 samples. The inclusions observed in the samples are both primary and secondary mono-phase & bi-phase. Carbonic inclusions are dominantly mono-phase although few bi-phase carbonic inclusions have also been noticed. Secondary inclusions are smaller which show rounded, sub-rounded and faceted shapes and have been seen along healed fractures in linear fashion. Trails of very fine inclusions also are observed. Primary bi-phase inclusions are too small to use. The size of the vapour phase in the form of bubble ranges in size from 0.070 to 1.887 μm. The size of workable bi-phase aqueous-vapour inclusions varies from 4.2 μm to 11.15 μm. Observation after Micro thermometry of Bi-phase aqueous-vapour inclusions [63] [64] .

Te which is the initial melting temperature ranges from 20.2˚C to −31.2˚C with an average of −25.7˚C which indicates presence of NaCl ± KCl salt in the fluid inclusion assemblage and it has also been observed that the major dissolved component in the aqueous phase is NaCl and attributes to a compositional system of NaCl-H₂O ± KCl for the fluids.

T_fice which is the final ice melting temperatures of the aqueous phase in these inclusions vary between −0.2˚C and −2.9˚C with an average value of −1.5˚C simply indicates that the fluid is marginally saline.

T_h (homogenization temperature): Three different sets of range of homogenization temperature (T_h) of the aqueous vapour rich fluid inclusions have been found:

1^st set - 134.8˚C to 150.5˚C (average 142.65˚C).

2^nd set - 169.8˚C to 182.3˚C (average 176.05˚C).

3^rd set - 205.6˚C to 220.1˚C (average 212.8˚C).

Salinity is 0.33 to 4.54 wt% NaCl equivalent (average 2.435 wt% NaCl equivalent).

Density of the inclusions varies from 0.86 to 0.96 g/cm³.

Observation after Micro thermometry of Biphase aqueous-vapour inclusions: Carbonic inclusions are most likely heterogeneously trapped inclusions and that’s why they do not homogenize at the same temperature as the aqueous inclusions. The melting temperature of CO₂ ranges from −57.1˚C to −58.2˚C and the maximum depression of melting temperature of CO₂ is −58.2˚C which indicates the fluid contains only CO₂. These aqueous carbonic inclusions homogenized between −6.8.7˚C to 9.7˚C into liquid CO₂ phase. The fluid pressures vary from 1.9 kbar to 2.5 kbar.

The temperature of homogenization vs. salinity plot of aqueous-vapour fluid inclusion suggests mixing between “main fluid” and cooler fluids/heated meteoric water possibly of same salinity. Hence, it may be concluded that the high temperature populations of isochore (205.6˚C to 220.1˚C) main fluid when this fluid enters into the host rock, because of pressure reduction the fluid starts boiling which is indicated by 169.8˚C to 182.3˚C isochore. 134.8˚C to 150.5˚C isochore indicates mixing of cooler fluids/heated meteoric water possibly of same salinity with the main fluid.

The studies were carried out from Baniwalaki Dhani, [53] by collecting a large number of samples from various depths and various modes of sulphide occurrence. Their findings are as follows from the northern part of the belt in Baniwala ki Dhani block.

1) The moderate to high saline gas poor fluids were responsible for Cu-Ag mineralization in the area.

2) The homogenization temperature ranged between 130˚C to 375˚C with average temperature of entrapment being 250˚C to 300˚C.

3) The fluids were emplaced at a pressure of 1.7 Kb and exhibit a mixing with the slight cooler fluids during emplacement.

4) The ore textures and sulphide phases however are indicative of entrapment temperature of the order of 500˚C, indicates extraneous heat source probably a granitic intrusion.

While comparing the fluid inclusion data of both the blocks following observations/interpretations can be made.

1) There is difference in the range of temperature of entrapment/homogenization, the elevated temperature in Baniwala could be due to the fact that there might have been more epigenetic component of mineralization at the expanse of some pegmatitic intrusions, as the association of Molybdnite has been noticed only from Baniwala ki Dhani block.

2) There is marginal difference in salinity of the fluids in both the blocks. The Baniwala ki Dhani fluid studies point towards a moderate to high saline fluid, while the Nanagwas area fluids suggest only marginally saline fluids. This again either can be due to the fact that the population studied in case of Nanagwas is only secondary inclusions suggesting there by that it represents only a subordinate event may be associated with the deformation and not exactly with the entrapment of fluid or these two blocks have mineralization emplaced at different stage of deformation.

3) Besides these two anomalies the average fluid entrapment temperature appears to be the same in both the blocks which is 130˚C to 220˚C and non-isothermal mixing of hot aqueous fluid with cooler fluid has been recorded in both the cases.

4) The above situation/anomalies could be explained by convective hydrotherms which is a rule rather than exception in the strata-bound deposits. The fact that silver is restricted to the Baniwala-Dokan area supports this observation, as the comparatively higher gradient of temperature in the deeper part will facilitate deposition of silver in association with chalcocite as per the paragenitic sequence of deposition of sulphides in a sedimentary basin, which goes Chalcocite-bornite-chalcopyrite-Pyrite/Pyrrhotite and Hematite from the deeper parts outward.