Ophiolites components occur in Pan-African belt in Central Eastern Desert(CED)and South Eastern Desert(SED.The ultramafic components are severely serpentinized and in some areas occur as small fresh
The Precambrian podiform chromitites associated with ophiolites are abundant in Pan-African belt in central Eastern Desert(CED)and south Eastern Desert(SED),Egypt and range from 690 to 890 Ma in age.The studied chromi...The Precambrian podiform chromitites associated with ophiolites are abundant in Pan-African belt in central Eastern Desert(CED)and south Eastern Desert(SED),Egypt and range from 690 to 890 Ma in age.The studied chromitites associated with Neoproterozoic ophiolites are distributed in southern Eastern Desert,Egypt in Baranis-Shalaten sheet and occur as lenticular bodies with variable dimensions in ultramafic component(serpentinites).We present geochemical and mineralogical data from three areas of ophiolites and associated chromitites namely Gebel Abu Dahr(D),Gebel Arais(A)and Gebel Anbat in the Wadi Hodein area(H)(Fig.1).The paper studies the compositional variations and tectonic settings of podiform chromitites associated with ultramafic rocks,in addition to the alteration process of chromite during metamorphism.The ophiolite in the present areas is composed of the ultramafic rocks(mainly serpentinites)with minor relics of fresh dunite and harzburgite.All these rocks are affected by metamorphism and subsequent retrograde during subduction and exhumation.Six samples selected from the serpentinites geochemically analyzed for major,trace and some REE elements and the geochemical results reflect that harzburgite and dunite compositions are typical of depleted mantle peridotite.Microprobe analyses and SIMS investigations were carried out for three massive podiform chromitite ore bodies and disseminated chromites in serpentinites(1215 spot probe analyses),and silicate minerals in serpentinite rocks such as serpentine and olivine(102 spots).Serpentine minerals are mainly antigorite with some chrysotile in serpentinite rocks and in chromitites,mainly filling cross-cutting veins.In this study,we consider that the alteration occurred in two stages:during the first one chromite reacted with olivine and water to form Cr-and Fe-rich,porous chromite and chlorite;during the second event magnetite filled the pores,created in the porous chromite and defused into this chromite to form homogeneous magnetite.According to this,the composition of chromite is a key factor controlling the metamorphic reaction between olivine and chromite because if the primary chromite is very poor in Al,the chlorite-forming reaction hardly takes place.In this case,during the second event,the addition of magnetite only contributes to create a magnetite corona around the former chromite grains without any diffusion at the chromite-magnetite boundary as suggested by Gerbilla et al.(2012).Barnes(2000)studied the chromite in komatiites and modification during green schist to mid amphibolite facies metamorphism.He suggested that the chromite cores continually equilibrated with magnetite rims document metamorphic grade conditions.Barnes(2000)suggested that the relative proportions of Cr3+,Al3+and Fe3+of chromite are not affected by metamorphism up to lower temperature amphibolite facies implying restricted mobility of these elements occurred under lower amphibolite facies.So,the chromite in lower temperature amphibolite facies preserves its primary igneous chemistry and can be used to estimate the metamorphic grade.Sack and Ghiorso(1991)and Barnes(2000)suggested that all chromite cores are equilibrated at temperature below^500–550℃corresponding to lowest amphibolite facies metamorphism and reflect magmatic composition not influenced by metamorphism.In this study,there is no alteration but only nearly pure magnetite deposition and development with restricted Cr-solubility at<500℃in the chromite rims on crystal boundaries and within fractures as shown in Fig 2a,b.Also magnetite alters later to hematite.The podiform chromitites are common in the Moho transition zone(MTZ)to the mantle section of ophiolites or harzburgite dominant peridotite massifs(e.g.,Arai,1997;Miura et al.,2012).They have been interpreted as a product of peridotite/melt reaction and subsequent melt mixing within the MTZ to the upper mantle;they are basically magmatic cumulates that formed at the upper mantle level(e.g.,Arai and Yurimoto,1994;Zhou et al.,1994).They are thus a good marker of peridotite/melt reaction(e.g.,Arai,1997).The Pan-African podiform chromitites mayh ave formed in the same way as the Phanerozoic,namely by melt-harzburgite reaction and subsequent melt mixing.The podiform chromatites and disseminated chromites are high-Cr chromites and have range in Cr#(Cr/Cr+Al)atomic ratio from 0.75 to 0.95 and low Ti with boninitic affinity(Fig.3a),indicating an island arc setting in supra-subduction zone setting.The present massive chromitites and disseminated chromites in serpentinites fall in the field of chromites de Bou Azer,chromites de Cordoba,Argentinia in the Cr#versus Mg#diagram(Fig.3 b,c)(Gervilla et al.,2012)The studied chromatites contain some grains of platinumgroup minerals(PGM)such as sulfides(Os-rich laurite)and Os–Ir alloy as shown in Fig.4 and as reported in South Eastern Desert by Ahmed(2007).展开更多
The Neo-Proterozoic ophiolites occur in the central and southern Eastern Desert along suture zone as dismemberedmassesinvolcano-sedimentary assemblages.The ophiolite component includes ultramafic rocks mainly serpenti...The Neo-Proterozoic ophiolites occur in the central and southern Eastern Desert along suture zone as dismemberedmassesinvolcano-sedimentary assemblages.The ophiolite component includes ultramafic rocks mainly serpentinites,mafic rocks,minor bodies of trondhjemite,sheeted dykes,metabasalts,and pillow lavas.The Present studies include two ophiolites in Central and southern eastern Desert named Mubarak–El Mayet and Ghadir respectively(Fig.1).The first one named after wadi Mubarak and wadi El Mayet area(55 km north Marsa Alam city)and the second named after Wadi Ghadir(30 km south Marsa Alam city).The dismembered ophiolite components in MubarakEl Mayet mainly composed mainly of serpentinites,ophiolitic metagabbros,sheeted dykes and Pillow lavas.All components occur as thrusted blocks and sheets in metavolcano-sedimentary assemblages(matrix).Gabbros sometimes occur as coarse grained gabbros(appenites)whereas pillows range in size from 30 cm to 1 m(Fig.2a).The second ophiolite sequence expose in Wadi Ghadir and its tributary.It consists of serpentinized peridotites,layered gabbro,massive isotropic gabbro,1fine grained gabbro,sheeted diabase dykes,pillowed basaltic lavas and minor plagiogranites.The serpentinizedperidotites,metapyroxenitesand serpentinites occur as allochthonous dismembered blocks,fragments and sheets in highly sheered metasediments and metavolcanics(mélange)(Fig.2b,c).The massive and layered gabbros occur in the main wadi(Fig.2d,f)and in many places contain some veins and pockets from plagiogranites.The present gabbros intruded by syenogranites from the east.Pillow lavas occur between metasedimentary mélange and ophiolitic gabbros in wadi El Beda as tributary of Wadi Ghadir and sometimes occur as fragments in mélange.The pillows range in size from 40 cm to 1 m(Fig.2f)and are mainly amygdaloidal and porphyritic basalt and spilite.Sheeted dykes cut the gabbros and pillow lavas in the Wadi El Beda and composed mainly from diabase(Fig.2g,h).In the present study,47 samples for major,trace and REE elements from different rock types in Mubarak-El Mayet(18 samples)and Ghadir ophiolite(29 samples)were analyzed.The field work and the geochemical data will discussed in the present work to evaluate the tectonic setting,origin and mantle source for two ophiolite suites.展开更多
Precambrian ophiolites are abundant in the Arabian- Nubian Shield of NE Africa and Arabia and range in age fronl 690 to 890 Ma. In Egypt, they are widely distributed in the central and southern Eastern Desert and occu...Precambrian ophiolites are abundant in the Arabian- Nubian Shield of NE Africa and Arabia and range in age fronl 690 to 890 Ma. In Egypt, they are widely distributed in the central and southern Eastern Desert and occur as nape complexes along sature zone or dismembered masses in rnetavolcano-sedirnenatry assemblages.展开更多
文摘Ophiolites components occur in Pan-African belt in Central Eastern Desert(CED)and South Eastern Desert(SED.The ultramafic components are severely serpentinized and in some areas occur as small fresh
文摘The Precambrian podiform chromitites associated with ophiolites are abundant in Pan-African belt in central Eastern Desert(CED)and south Eastern Desert(SED),Egypt and range from 690 to 890 Ma in age.The studied chromitites associated with Neoproterozoic ophiolites are distributed in southern Eastern Desert,Egypt in Baranis-Shalaten sheet and occur as lenticular bodies with variable dimensions in ultramafic component(serpentinites).We present geochemical and mineralogical data from three areas of ophiolites and associated chromitites namely Gebel Abu Dahr(D),Gebel Arais(A)and Gebel Anbat in the Wadi Hodein area(H)(Fig.1).The paper studies the compositional variations and tectonic settings of podiform chromitites associated with ultramafic rocks,in addition to the alteration process of chromite during metamorphism.The ophiolite in the present areas is composed of the ultramafic rocks(mainly serpentinites)with minor relics of fresh dunite and harzburgite.All these rocks are affected by metamorphism and subsequent retrograde during subduction and exhumation.Six samples selected from the serpentinites geochemically analyzed for major,trace and some REE elements and the geochemical results reflect that harzburgite and dunite compositions are typical of depleted mantle peridotite.Microprobe analyses and SIMS investigations were carried out for three massive podiform chromitite ore bodies and disseminated chromites in serpentinites(1215 spot probe analyses),and silicate minerals in serpentinite rocks such as serpentine and olivine(102 spots).Serpentine minerals are mainly antigorite with some chrysotile in serpentinite rocks and in chromitites,mainly filling cross-cutting veins.In this study,we consider that the alteration occurred in two stages:during the first one chromite reacted with olivine and water to form Cr-and Fe-rich,porous chromite and chlorite;during the second event magnetite filled the pores,created in the porous chromite and defused into this chromite to form homogeneous magnetite.According to this,the composition of chromite is a key factor controlling the metamorphic reaction between olivine and chromite because if the primary chromite is very poor in Al,the chlorite-forming reaction hardly takes place.In this case,during the second event,the addition of magnetite only contributes to create a magnetite corona around the former chromite grains without any diffusion at the chromite-magnetite boundary as suggested by Gerbilla et al.(2012).Barnes(2000)studied the chromite in komatiites and modification during green schist to mid amphibolite facies metamorphism.He suggested that the chromite cores continually equilibrated with magnetite rims document metamorphic grade conditions.Barnes(2000)suggested that the relative proportions of Cr3+,Al3+and Fe3+of chromite are not affected by metamorphism up to lower temperature amphibolite facies implying restricted mobility of these elements occurred under lower amphibolite facies.So,the chromite in lower temperature amphibolite facies preserves its primary igneous chemistry and can be used to estimate the metamorphic grade.Sack and Ghiorso(1991)and Barnes(2000)suggested that all chromite cores are equilibrated at temperature below^500–550℃corresponding to lowest amphibolite facies metamorphism and reflect magmatic composition not influenced by metamorphism.In this study,there is no alteration but only nearly pure magnetite deposition and development with restricted Cr-solubility at<500℃in the chromite rims on crystal boundaries and within fractures as shown in Fig 2a,b.Also magnetite alters later to hematite.The podiform chromitites are common in the Moho transition zone(MTZ)to the mantle section of ophiolites or harzburgite dominant peridotite massifs(e.g.,Arai,1997;Miura et al.,2012).They have been interpreted as a product of peridotite/melt reaction and subsequent melt mixing within the MTZ to the upper mantle;they are basically magmatic cumulates that formed at the upper mantle level(e.g.,Arai and Yurimoto,1994;Zhou et al.,1994).They are thus a good marker of peridotite/melt reaction(e.g.,Arai,1997).The Pan-African podiform chromitites mayh ave formed in the same way as the Phanerozoic,namely by melt-harzburgite reaction and subsequent melt mixing.The podiform chromatites and disseminated chromites are high-Cr chromites and have range in Cr#(Cr/Cr+Al)atomic ratio from 0.75 to 0.95 and low Ti with boninitic affinity(Fig.3a),indicating an island arc setting in supra-subduction zone setting.The present massive chromitites and disseminated chromites in serpentinites fall in the field of chromites de Bou Azer,chromites de Cordoba,Argentinia in the Cr#versus Mg#diagram(Fig.3 b,c)(Gervilla et al.,2012)The studied chromatites contain some grains of platinumgroup minerals(PGM)such as sulfides(Os-rich laurite)and Os–Ir alloy as shown in Fig.4 and as reported in South Eastern Desert by Ahmed(2007).
文摘The Neo-Proterozoic ophiolites occur in the central and southern Eastern Desert along suture zone as dismemberedmassesinvolcano-sedimentary assemblages.The ophiolite component includes ultramafic rocks mainly serpentinites,mafic rocks,minor bodies of trondhjemite,sheeted dykes,metabasalts,and pillow lavas.The Present studies include two ophiolites in Central and southern eastern Desert named Mubarak–El Mayet and Ghadir respectively(Fig.1).The first one named after wadi Mubarak and wadi El Mayet area(55 km north Marsa Alam city)and the second named after Wadi Ghadir(30 km south Marsa Alam city).The dismembered ophiolite components in MubarakEl Mayet mainly composed mainly of serpentinites,ophiolitic metagabbros,sheeted dykes and Pillow lavas.All components occur as thrusted blocks and sheets in metavolcano-sedimentary assemblages(matrix).Gabbros sometimes occur as coarse grained gabbros(appenites)whereas pillows range in size from 30 cm to 1 m(Fig.2a).The second ophiolite sequence expose in Wadi Ghadir and its tributary.It consists of serpentinized peridotites,layered gabbro,massive isotropic gabbro,1fine grained gabbro,sheeted diabase dykes,pillowed basaltic lavas and minor plagiogranites.The serpentinizedperidotites,metapyroxenitesand serpentinites occur as allochthonous dismembered blocks,fragments and sheets in highly sheered metasediments and metavolcanics(mélange)(Fig.2b,c).The massive and layered gabbros occur in the main wadi(Fig.2d,f)and in many places contain some veins and pockets from plagiogranites.The present gabbros intruded by syenogranites from the east.Pillow lavas occur between metasedimentary mélange and ophiolitic gabbros in wadi El Beda as tributary of Wadi Ghadir and sometimes occur as fragments in mélange.The pillows range in size from 40 cm to 1 m(Fig.2f)and are mainly amygdaloidal and porphyritic basalt and spilite.Sheeted dykes cut the gabbros and pillow lavas in the Wadi El Beda and composed mainly from diabase(Fig.2g,h).In the present study,47 samples for major,trace and REE elements from different rock types in Mubarak-El Mayet(18 samples)and Ghadir ophiolite(29 samples)were analyzed.The field work and the geochemical data will discussed in the present work to evaluate the tectonic setting,origin and mantle source for two ophiolite suites.
文摘Precambrian ophiolites are abundant in the Arabian- Nubian Shield of NE Africa and Arabia and range in age fronl 690 to 890 Ma. In Egypt, they are widely distributed in the central and southern Eastern Desert and occur as nape complexes along sature zone or dismembered masses in rnetavolcano-sedirnenatry assemblages.
