Research on Altered Granites

Research on Alte expiration GranitesVisible jaundiced radial U- minerals (up to 1 % U )was recorded coating the fractures in the she ard granites, knell on the 2 sides by milky watch crystallization veins, which gyp as septa for U- minerals migration. From the mineralogical point of view, the trimed granite plenteous in a) uranium (meta-autunite, kasolite and phurcalite) , b) thorium (uranothorite) and c) innovation alloys (wolframite, columbite, fergusonite and Plumbopyrochlore minerals) in addition to zircon, allanite, rutile, fluorite, fluro-apatite, phlogopite and bid oxide minerals (hematite, ilmenite, goethite and magnetite )(Table.1).Meta-autunite occurs as lemon-yel mild to greenish yellow, subhedral crystals miscellanyed as dehydration pseudomorphs after autunite (Fig,6a) and usually associated with kasolite. Phurcalite occurs as light brown subhedral to anhedral crystals of calcium uranium phosphate (Fig,6b) and usually associated with push oxides.The alter g ranites are enriched in most major oxides (Fe2O3, Tio2, ,Mn, Mg, CaO and P2O5,) pull out SiO2 and Na2O than sporting granites (Fig.7) manifesting ferrugination, calcification ,desilicification and illitization .Also the refreshed granites are depleted in most decode elements (Ni, Cr, Sr, Zr, Y, Ga, Zn, Pb, and Cu) except Nb than alte release geniuss. Based on major element data, the main(prenominal) characteristic features of the studied alte going granites are highschooler in Fe/Mg ratio (15 av.), lower in SiO2(av.52.8 %)andNa2O /K2O ( av.0.16) than fresh granites Table 2 ) .Fig. 6 Photomicrographs showing a) meta-autunite crystal surrounded by phurcalite mineral in alte loss granites. C.N., X=40 and b) phurcalite mineral associated with straighten out oxide in altered granites. C.N., X=40.Table (1) Shows the core of minerals occurrences in the study area.Minerals group fluctuate typesMineralsUranium minerals change granite Meta-autunite, Phurcalite and KasoliteThorium mineralsUranothoriteBase MetalsAltered graniteWolframiteinkiness JasperCassiterite, Wolframite, Zincite, Ni-chromite and Cr-spinelRed JasperNi-Chromite and Cr-spinel whitish quartzGalena, Pyrite, pyrrhotite and SphaleriteCopper Mineralsmilky quartzcovellite, borniteRed Jaspercrysocolla abusive JasperAtacamite, Paratacamite, and cuprite Native mineralsBlack Jasper and Milky quartzGold and NickelNb-Ta mineralsAltered granitesPlumbopyrochlore, Columbite and FergusoniteREEs-Bearing MineralsAlkali felspar granitesZircon, FluoritesyenogranitesZircon, allaniteAltered granitesZircon, Allanite, Rutile and FluoriteStream sedimentsZircon, MonaziteBlack JasperXenotimeRed Jasper press MineralsAltered granitesHematite, Ilmenite, Goethite and magnetiteBlack JasperHematite, MagnetiteRed JasperHematite, Magnetite and GoethiteMilky quartzHematiteFig.( 7 ) The enrichment and depletion of major oxides and trace elements of altered granites to the fresh granites samples.Fig.( 8 ) Bar- diagram showing th e trace elements distribution of red and relentless jasper.The content of HFSE in both fresh and altered granites (Nb (36-10 ppm), Zr (316- 759 ppm), Y(69- 220 ppm) ,U (8-ppm) respectively as well as low Rb/Sr ratio (1.04-0.45) and K/ Rb ratio (0.03-0.04) (Table 2) suggest that the fresh granites are primarily derived from felsic cum .On the opposite side, these criteria in the altered granites are critical for uranium geographic expedition . The drab jasper more richer than red cardinal in Ni (av.1004 -81ppm),Cr(av.8575 -853ppm),Zn (av.144 -80 ppm), Cu(av.1106- 35 ppm), Co(av.371-0.0 ppm), Au(1.04 -0.5 ppm) and U(40- 8800ppm)respectively (Table 2,Fig.8 ).The latest event invades the WNW-ESE rob regularise was the intrusion of silica and jasper veins with dissentent magnitude. The excess of released quartz can immigrate as colloidal silica to precipitate later in the tension fractures as jasperoid vein at upper geomorphological levels under low temperature condition .Sil icification on the main overcharge zone has a perceptible amount of liberated secondary silica occurs as fine crystals associated with the great primary quartz crystals and characterized by the existence of three generations of silica veins differ in touch, mineralization and age.1)The milky quartz veins are the first degree (the youngest one), in the first place barren, running WNW and dipping 70/ sou-sou-west direction, highly brecciated (2-5 Km in duration, 0.25-3 m in width)and frequent only at the southern border of the shear zone.2) The red jasper veins(second phase) have E-W ,WNW,NW and NE trends (Fig.5), dipping 50-75/N or S , 45/ SSW, SW and SE direction respectively. They fractured, fragmented, discontinuous, brecciated,(7km in length, 0.30-3 m in width) and rich in Cr, , Ni, Sn, Zn and Cu- mineralization (Fig.6) (some parts of red jasper are rich by vugs (physical tap) that are filled by mineralization. These veins exhibit combinations of more than one style orbi cular and brecciated. Brecciated red jasper (Plate 4.a) can vary from soft swirls of color to dramatically fragmented shades of rich brown, brick red and cream colors. deeply integrated colors come from organic materials and iron oxides imbedded in the stones.Ore microscopical investigation reveals that quartz crystals occur as anhedral crypto limpid associated and stained by iron oxide. Sometimes cryptocrystalline crystals of amorphous silica form banding. Iron oxide occurs as black crystalline minerals and staining of quartz.3) The black jasper(oldest one) is be by 1.8 km in length, 0.5-10 m in width, trending N45W ,dipping 50-65 /SW (Figs.5), and rich in Cr, Ni, Cu and Au mineralization, Fig.7).They are concentrated only in the east part of G. Um Bakra shear zone and less abundant in length than milky and red veins. The black jasper are vuggy than milky and red silica veins and these vugs filled by calcite minerals. The apical parts of the veins are intensely weathered, oxidize d, brecciated fragments (Plate.4b) and decomposed to forming gossans.Petrographically, quartz occurs as cryptocrystalline and polycrystalline forming spherulitic texture and associated with iron oxide. Iron oxide associated with quartz and sometimes forming network or needle (Plate .4c). Cr- spinel with blood red color was spy and having darker boundaries with quartz (Plate.4d).Ore microscopic study reveals the presence of gold, chromite and magnetite minerals. Fire examine for gold content give 1.04 g/ton .Chromite occurs as anhedral crystal associated with magnetite (Plate.4e). Chromite existed in different forms zoned veinlet or disseminated specks (Plate. 4 fg). Black minerals weft fracture and associated with quartz (Plate.4h) .Fig. (6) showing different types of copper minerals in red and black jasper ,a) atacamite mineral, b) paratacamite mineral, c) cuprite mineral and d) crysocolla mineral .Fig. (7) Photograph showing copper minerals from black jasper of the study area.Al terationsTwo phases of hydrothermal alterations acid and alkaline were distinguished in the shear zone resulting in Kaolinization and ferrugination processes as illustrated belowKaolinization indicates that the trembles were affected by sulfurous root word with low temperature varying from 200 to 250 C (Helgeston 1974). Kaolinitization process causes an plus in alumina (18.2%) at the expense of the other major oxides (Table2).Kaolinization affects shear granites in the shear zone are characterized by the formation of ashes minerals and adsorbed secondary U- minerals( meta-autunite, Kasolite and Phurcalite) (Table1).Acidic alteration of biotite spring ups illite+quartz ,while magnesium, iron, oxygen, and fluorine are fade away in hydrothermal precariouss (Pirajno,1992). These solution caused the alteration of the feldspars and micas to clay minerals (Fig.8) are produced by an acid-forming fluid and it liberates silica and K+ according to Pirajno,(1992). Similarly, the anor thite component of plagioclase is modify to (clay minerals) (Hemley and Jones, 1964 Pirajno1992) and frees Ca2+ ions transported also by the hydrothermal solution. The free Al+3 increase the alumina in the clay mineral. This kind of alteration by acid solution is responsible for transported and redeposited uranium and base alloys mineralization in WNW-ESE shear zone which acts as a good trap.carbonitizationThe common presence of calcite manifesting carbonitization process along the shear zone (Fig.8).Also both of ultramafic -mafic oscillates and intrusive gabbros are rich by revision minerals.Ferrugination causes increase in total Fe2O3 content (FeOt= 4.7%. to 32.7%) at the expense of other oxides. The strong alkaline solution may precipitate Fe+3 and U+6 within the shear zones in the form of iron oxy-hydroxides rich in uranium (Cuney, et al., 1984). Sheared granite samples stained by Fe oxides adsorb U minerals at the main shear zone. Ferrugination is represented mainly by h ematite and goethite minerals (table1, Fig.9).Oxygen may combine with iron to produce hematite forming hematitic alteration.Plate 4 Photomicrographs showing a) brecciated red jasper vein, C.N., X=40., b ) brecciated black jasper vein with vugs, c) black silica vein showing hematitization in quartz, iron oxide occurs as needles in quartz. C.N., X=40, d) blood red, Cr spinel having darker boundaries in BJV (PPL), X=20., e) chromite (cr) in rim and magnetite (mag) in core in BJV. X =40, f) veinlet of chromite and groundmass of magnetite in BJV. X=40, g) disseminated specks of chromite in BJV. X= 40, h) red jasper vein showing iron oxide present as black crystalline minerals and staining of quartz. C.N., X=20fluoritization Fluorite was emplaced through the fractures and fissures in altered granite along the shear zone. The released 3Ca2+and 6 F during illitization of the anorthite and biotite may combine in concert forming fluorite which is observed within the shear zone associate with U- minerals.AcknowledgementsOur true(prenominal) thanks and gratitude should be provided to Dr.I, Hassan and Dr.W. El-Gazlawy, NMA, for their help during field work.Discussion Conclusion1-To form a hydrothermal deposit in Um Bakra- Um Samra WNW-ESE shear zone requires (1) a magma source of fluid, (2) dissolved metals in the magmatic fluids, , (3) heat source and activate tectonic, causes the migration of uid and (4) Presence of hold ways, layering and physical cavities, to precipitates the metals or minerals.2-G. Um Samra -G. Um Bakra shear zone strikes N-80 and dipping 45 /SSW and ranges from 30 to 500 m in thickness and extends 10 km in length. The host rock (syenogranites)is highly altered, fine -grained,ferruginous ,reddish ping and grayish pink to grayish in color. Two opposite N-S strike-slip faults and NNE and NNW strike-slip faults dextral and sinistral sense of movement(good channel ways) forming grabben and horst structures respectively (6 km in length, 30 m in width, d ipping 10-20 towards E or W) cut the shear zone.3-Three generations of silica veins differ in color, mineralization and age are common. The first phase (youngest),is barren milky quartz veins, running WNW and dipping 70/ SSW direction , highly brecciated (2-5 Km in length, 0.25-3 m in width. The red jasper(second phase) has N 60-76 W trend, dipping 45/ SSW direction, fractured, fragmented, discontinuous, brecciated, (7km in length, 0.30-3 m in width) and rich in Cr, Ni, Sn, Zn and Cu- mineralization) .The third phase (oldest one) is represented by black jasper (1.8 km in length, 0.5-10 m in width, trends N75W ,dipping 50-65 /SSW and rich in Cr, Ni, and Au mineralization).4-The black jasper more richer than red one in Ni (av.1004 -81ppm),Cr(av.8575 -853ppm),Zn (av.144 -80 ppm), Cu(av.1106- 35 ppm), Co(av.371-0.0 ppm), Au(1.4 -0.5 ppm) and U(av, .ppm)respectively (Table ).5-The presence of clay mineral (dickiteAl2Si2O5(OH)4) in quartz and jasper veins indicates a temperature environme nt higher than 200C. The fuse of volatile fluids with meteoric water and fluid- wall rock interaction result in changes in pH and oxygen activity and deposition of base metals.6- Precipitation of hematite in shear zone and red jasper veins believably decreased the pH of the solution and rising acidic fluids. The sudden change in the pH and temperature of the fluids will lead to destabilization of base metal complexes favouring their deposition (Alexandrov et al., 1985).7-The cooling of the hydrothermal solution decreases the solubility of the metals. Cooling can use up place when hot magmatic uids enter cooler wall rocks or when two uids mix, Similar reactions can take place between hydrothermal solutions and wall rock a solution containing dissolved sulde might contact a rock containing magnetite, to convert the magnetite to iron pyrite by a process called suldation.Or, a solution containing Cu might react with a rock containing pyrite to form Cu suldes.8- The base metals miner alization are accumulate in the repose melt of the late fractionate alkali feldspar granites (Bright, 1974) especially upwards in the magmatic system (Smith,1979). During the emplacement of the basic and intermediate dikes (olivine basalt, andesite and dolerite dikes) which accompanied with high temperature and Co2), the base metals(galena, pyrite, sphalerite and cassiterite) were precipitated from saline and reduced fluids as sulfides due to cooling, fluid combine and wall rock reaction.9-The banded texture in jasper veins is common in epithermal base metals, indicating of boiling event and rapid deposition (Hedenquist et al.,1995).Most epithermal deposits lie down of numerous separate, largely vertical veins that form a conjugate set, sometimes reecting regional tectonic stress. Low-temperature hydrothermal solutions (10- The non-sulfide ore deposits are classified into two major types supergene and hypogene deposits (Hitzman et. al., 2003). (a) Supergene deposits form primari ly from the oxidation of sulfide-bearing deposits and are formed principally zinc carbonate or silicates, and (b) hypogene deposits consist dominantly of zinc silicates and oxides, and they commonly result from mixing of a reduced, Zn-rich, with an oxidized, sulfur-poor fluid. Um Bakra-Um Samra shear zone containing zinc oxides (hypogene deposits).11-Pyrite presents in two generations, disseminated and along fractures. The occurrence of covellite, bornite and magnetite are related to the oxidation production of disseminated pyrite, whereas the second type of pyrite transformed into pyrrhotite.12-The chloritization process is the last phase of alteration in the shear zone, where fluids became rich in Mg/Fe most probably due to the decomposition of ferromagnesian minerals from the basic and intermediate dikes.Fig.( 8) wake Kaolinization map for Um Bakra -Um Samra area.Fig.( 9) showing ferrugination map for Um Bakra -Um Samra area.Table (2 ) chemical digest of major oxides and trac e elements of Um Samra-Um Bakra area.Trace elements (ppm)FreshAltered RedBlackNi flow0.0-550-180950-409314-1501 bonny102322811004Cr track down233-485113-2409294-26893490-12898 total2967988538575Rb range of mountains83-2100-3920.0-11610.0average147.1282890.0Sr honk17-50773-588-1270-17Average142278747Zr plod89-659196-18730-4660.0Average3167592380.0YRange16-10284-5120-790-142Average692203877NbRange14-560-620-350.0Average3610110.0GaRange22-450-1510-590.0Average3273240.0ZnRange16-1450-240932-16956-281Average7852880144PbRange0-520-6840-1730.0Average16157450.0CuRange0-320-2100-80431-2045Average426351107CoRange0.00.00.00-558Average0.00.00.0371MoRange0.00.00-1270.0Average0.00.0250.0AsRange0.00.00-20980.0Average0.00.04190.0URange0.00-76400.00.0Average0.017490.00.0Major oxides %FreshAlteredRedBlackSiO2Range69.22-75.3323.14-72.0970.3-92.5372.93-91.27Average72.952.884.282.7TiO2Range0.01-0.290.28-2.460.01-0.220.0Average0.21.080.20.0Al2O3Range12.35-15.410.37-18.020.69-14.850.69Average13.712.76.80. 8Fe2O3Range0.08-2.912.10-45-771.39-4.974.46-22.54Average1.919.83.413.4MnORange0-0.080-0.750.01-0.030.01-0.04Average0.030.10.030.03MgORange0.13-0.650.24-7.230.29-1.750.19-0.60Average0.311.320.8060.442CaORange0.45-2.551.26-4.40.31-0.760.01-1.74Average1.12.60.60.5Na2ORange3.15-4.340.12-3.340.05-2.20.05-0.12Average3.70.80.60.08K2ORange4-6.701.84-7.780.1-6.960.04-0.09Average5530.06P2O5Range0.020.160.01-1.230.07-0.480.02-0.04Average0.080.390.2240.032L.O.I.Range0.04-0.850.8-2.80Average0.311.43 chalk upRange99.73-99.993.22-99.9199.36-99.9297.45-99.01Average10098.4299.798.288ReferencesAbdalla, H. 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