内蒙古查干花斑岩钼矿床：俯冲改造的富集型源区及碰撞后伸展环境对成矿的贡献
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摘要
查干花钼矿床位于内蒙古乌拉特后旗,是近年来发现的大型斑岩矿床,也是兴蒙造山带内众多斑岩型钼矿床中的一个典型。查干花矿区宏观地质单元主要由以下几个部分组成：宝音图群变质岩、“X”型断裂以及二叠纪多期次就位于宝音图群的二叠纪岩体。其中宝音图群是一套低角闪岩相至高绿片岩相的变质地层,构成了成矿岩浆就位前的基底；“X”型断裂是一组成矿岩体就位前形成的一组断裂,对后期成矿岩体的就位具有明显的控制作用；二叠纪多期次就位的岩体由早期中粗粒黑云二长花岗岩和晚期似斑状黑云母二长花岗岩组成。查干花斑岩钼矿化主要赋存于似斑状黑云母二长花岗岩体内,矿化蚀变主要有钾化、绢英岩化、硅化、粘土化和绿帘石化等,并由中心向外构成了明显的蚀变分带,辉钼矿化与绢英岩化、硅化具有密切关系。矿石主要呈细脉状和网脉状产出,部分具有大脉状特征。根据脉体形态和形成时间,可以主要可以分为成矿前的石英脉、成矿期主阶段石英-辉钼矿-绢云母脉、成矿期晚阶段石英-黄铁矿-绢云母脉、石英-辉钼矿脉、石英-黑钨矿脉及成矿期后石英-黄铁矿脉。
锆石LA-ICP-MS U-Pb测年结果显示,宝音图群黑云斜长角闪岩中挑选的锆石206Pb/238U年龄大部分位于464±5Ma-698±8Ma之间,少量古老锆石207Pb/206Pb可达1995±11Ma.二云石英片岩中挑选的锆石207Pb/206Pb年龄大部分位于1135±91Ma-1890±13Ma之间,少量年轻的锆石206Pb/238U年龄可以低至633±8Ma。结果表明宝音图群的原岩的沉积时代可以低至早古生代。侵入于宝音图群并随宝音图群一起变形变质的二长花岗岩的侵位年龄为446.4±1.OMa,变形变质年龄为399.4±1.5Ma,显示宝音图群的变形变质作用可能持续到早泥盆世。结合宝音图群主微量元素的分析显示,宝音图群的原岩应为沉积岩,其中角闪岩、斜长角闪岩可能为泥质、白云质沉积岩,二云石英片岩为石英含量不等的碎屑岩。二云石英片岩原岩的沉积环境可能为新元古代至古生代期间形成陆缘弧。
锆石SHRIMP U-Pb测年结果显示,早期黑云母二长花岗岩就位年龄约为273Ma,成矿期似斑状黑云母二长花岗岩就位年龄约为253Ma。矿区的岩浆活动构成了一个多阶段演化的,从早期逐渐增强至大规模岩浆上侵,随后衰减为小规模岩浆侵位,并伴随着大量成矿流体出溶的成矿岩浆活动周期。查干花斑岩钼矿化的发生是这个长期岩浆活动周期的结果。主微量元素和同位素研究显示,矿区内的两期花岗岩具有共同来源。主微量元素测试结果显示这两期花岗岩具有高度演化和分异的特征,是深部岩浆房内经历了一定程度结晶分异和同化混染的产物。这两期花岗岩也具有明显弧岩浆作用的特点,反映了深部岩浆源区可能受到了早期俯冲作用的改造,并在二叠纪期间的碰撞后伸展环境下就位。这两期花岗岩与兴蒙造山带内大量产出的新生的低(87Sr/86Sr)i高εNd(t)花岗岩具有明显的差异,(87Sr/86Sr)i变化范围较大,εNd(t)较低,显示上部地壳物质对岩浆的形成具有重要贡献,构成了成矿岩浆的地壳物质端元。同位素组成特征也显示受到了富集地幔EM1I的改造。
辉钼矿Re-Os同位素测年显示,斑岩钼矿化发生于～243Ma,晚于成矿期岩浆就位年龄近10Ma,是查干花成矿岩浆长期演化过程的反映,也与矿区地质特征相符。氢同位素组成具有明显的负值(δD可低至-133.9%0),硫同位素位于零值附近,但具有明显的正值(δ34S平均为2.97%0),显示成矿热液在岩浆中经历了明显的气液相瑞利分馏过程,也从侧面反映了成岩成矿过程的长期性。成矿期流体包裹体主要为气液两相H2O-NaCl体系,并含有少量的C02。测温结果显示,成矿期具有高均一温度(可高达387。C)和低盐度的特点。结合矿物对氧同位素温度计的研究结果,显示辉钼矿于653℃和200MPa (静岩压力深度7.4km)左右开始沉淀,并主要在384～416℃、40～65MPa(静水压力深度4-6.5km)环境下沉淀。矿床的形成与经历了明显去气作用的低盐度流体的长期演化有关,成矿流体气液相组分的分离是成矿系统内温度降低的重要原因,也是导致是辉钼矿沉淀的重要因素。矿床成矿期流体来源于岩浆,成矿物质的来源具有深部来源特征,可能来源于大陆下部岩石圈地幔及下地壳。
查干花矿床的地质特征和形成过程与伸展环境下高F型斑岩钼矿床具有明显的类似性,显示查干花斑岩钼矿床应属于高F型斑岩钼矿床。查干花也是兴蒙造山带内大型斑岩钼矿床(>10万吨)中最早形成者,其形成指示着兴蒙造山带内东西向-北东向大规模斑岩钼矿化的肇始。从查干花矿床的研究显示,晚古生代开始的碰撞后伸展构造环境及其控制下的高分异型岩浆活动对兴蒙造山带内大规模斑岩钼矿化的发生具有重要的贡献,但古生代期间的俯冲作用对矿床的形成同样具有重要意义。主要体现在以下几点：(1)塑造富集型岩浆源区.古生代期间的早期俯冲作用使得大陆岩石圈含有更高的地幔不相容元素(包括钼等成矿元素),进而构成成矿元素相对富集的大陆岩石圈；(2)水化造山带。早期的俯冲过程中的脱水熔融为兴蒙造山带输入了大量的水源,从而水化了造山带,为缺乏板块俯冲作用的碰撞后伸展环境中大规模斑岩钼矿化提供充足的成矿流体来源；(3)增厚大陆岩石圈。早期俯冲和碰撞过程使得兴蒙造山带形成加厚的大陆岩石圈,促进碰撞后伸展环境下岩石圈减薄,以及这个过程中的壳幔相互作用。
Located in Urat Rear Banner, Chaganhua is a typical and newly discovered large scale porphyry Mo deposit in Xing'an Mongolian orogenic belt. There are three main geological units occur in Chaganhua ore district:the Baoyintu Group metamorphic complex, the "X" shaped fractures and the Permian multistage intrusived granites. The Baoyintu Group metamorphic complex is medium-grade metamorphic rock and constitutes the main pre-ore basement. The Permian multistage intrusived granites is mainly composed of Early Permian biotite monzonitic granite and Late Permian porphyritic biotite monzonitic granite, the intrusion of later is controlled by the pre-ore "X" shaped fractures, and lead to the hydrothermal alteration and porphyry Mo mineralization of Chaganhua. The typical alteration includes potassic feldspathization, sericitization, silicification, argillization, epidotization and chloritization. The Mo mineralization is mainly hosted in porphyritic biotite monzonitic granite, and directly associated with the sericitization and silicification alteration. Most of the Mo mineralization occurs as vein and veinlet, based on the assemblage of alteration minerals of these vein and veinlet, they can divided into pre-mineralization quartz venlets, metallogenic quarzt-molybdnite-sericite venlets, quarzt-pyrite-sericite venlets, quarzt-molybdnite-venlets and quartz-wolframite vein and post-mineralization quartz-pyrite venlets.
LA-ICP-MS U-Pb dating study shows that most of zircons of plagioclase amphibolite from Baoyintu Group yield206Pb/238U ages ranging from464±5Ma to698±8Ma, and some of them yield207Pb/207Pb ages as old as1995±11Ma. Most of the zircons of two-mica quartz schist yield207Pb/207Pb ages ranging from1135±91Ma to1890±13Ma, and some of them yield206Pb/238U ages as young as633±8Ma. These ages show that the sedimentary time of the protolith of Baoyintu Group may as low as Middle Ordovician. The zircons from monzonitic granite which was deformated and metamorphic with Baoyintu Group yield two weighted mean concordant ages of446.4±1Ma and399.4±1.5Ma, these suggest that the monzonitic granite intruded the Baoyintu Group at Late Ordovician, and the time of metamorphism of Baoyintu Group may as low as Early Devonian. Incorporating the petrogeochemistry studies, we suggest that the protolithes of Baoyintu Group are sedimentary rocks, among which, the protolith of plagioclase amphibolite may be pelite mudstone, dolomite, and the protolith of two-mica quartz schist may be clastic rocks. These sedimentary may deposit in continental marginal arc formed in Late Proterozoic to Early Paleozoic.
SHRIMP U-Pb dating study shows that the pre-mineralization biotite monzonitic granite was emplaced at about273Ma, and the mineralization related porphyritic biotite monzonitic granite was emplaced at about273Ma.The emplacement of these granites constitute a long lived and multistaged magmatic evolution cycle, which was evolved from progressive magmatic activity to large-scale intrusion of granite, and waning to small-scale intrusion of ore forming magma, and to the exsolution of ore forming hydrothermal fluid. The mineralization activity is the outcome of this long lived magmatic evolution cycle. The petrogeochemistry studies suggest that these two granite intrusions share the same geochemical feature of highly evolved magma. We suggest that they are the consequence of AFC in the deep magma chamber under Chaganhua porphyry deposit, and their magma source was modified by the Paleozoic sudbuction of oceanic crust, and emplaced in Late Paleozoic extensional tectonic setting. The isotope chemistry studies show enriched feature for these granites, which are different from the low (87Sr/86Sr)i and high ε Nd(t) granites occurring Xing'an-Mongolia orogenic belt.We suggest that these granites are souced from two endmembers:upper crust and EMⅡ.
The molybdenite Re-Os dating show that the porphyry Mo mineralization occurred at about243Ma, which was about10Ma later than the emplacement of ore forming magma. This reflects a long duration of hydrothermal activity in Chaganhua deposit, which is agreed with the geological features of chaganhua deposit. These long duration are also supported by the stable isotopes studies, the ore forming fluid have very low δD (-133.9‰) and district positive δ34S (2.97‰), which show intense Rayleigh fractionation process of the ore forming fluid, and these also reflect a long evolution history of the ore forming fluid. Fluid inclusions in quartz of the main stage and late stage of molybdenum mineralization are mainly two phase vapor-liquid inclusions of H2O-NaCl composition with small amount of CO2phase. It's characterized by moderately low salinities and high homogenization temperatures. Combined with the studies of oxygen isotope thermometer, we suggest that molybdenum began to deposit at653℃,200MPa (approximately7.4km of lithostatic pressure) and mainly deposit at416℃to384℃,65MPa to40MPa (approximately6.5km to4km of hydrostatic pressure). The inclusions data combined with H-O isotope data record an evolution path of the hydrothermal fluid of degassed magma water source from high temperature, high pressure and moderately low salinity to low temperature, pressure and salinity which form Chaganhua porphyry molybdenum deposit, and these studies also suggest that the long fractionation history of ore foming fluid may be one of the important reasons for deposition of molybdnite. The H-O-S-Pb isotope geochemical studies also thow that the ore forming fluid are sourced from magmatic activity, and the ore forming substances are sourced from deep magma, and probably from subcontinental lithospheric mantle and lower crust.
The geology and metallogenic studies show that Chaganhua porphyry Mo deposit are comparable to the high F type porphyry Mo deposits occurs in extensional tectonic setting, and suggest Chaganhua is a high F type deposit. Chaganhua is also the oldest large scale porphyry Mo deposit occurring in Xing'an-Mongolia orogenic belt, its formation means the begining of extensive porphyry Mo mineralization along the S-E to NE trending Xing'an-Mongolia orogenic belt. The activity of highly evolved and differentiated magma in post-collision extensional setting may be of great significance, but the Paleozoic subduction-modified fertile magma source may also play a crucial role in the formation of these huge porphyry Mo mineralization belt as follows:(1) Building up the fertile magma source by subduction fluids enriched in incompatible elements in Paleozoic;(2) hydrating the orogenic belt by dehydration melting of subduction fluids in Paleozoic and this highly concentrated wate will be released in the post-collision extensional setting stage, and will contribute the huge volumes of ore forming fluid needed in the formation of this huge porphyry Mo mineralization belt in Xing'an-Mongolia orogenic belt;(3) Thickening the continental lithosphere in by subduction tectonism, the instability of this thickened lithosphere would thin again because of the termination of compressive stress in post-collision extensional setting, which will cause the extensive Crust-mantle interaction.
锆石LA-ICP-MS U-Pb测年结果显示,宝音图群黑云斜长角闪岩中挑选的锆石206Pb/238U年龄大部分位于464±5Ma-698±8Ma之间,少量古老锆石207Pb/206Pb可达1995±11Ma.二云石英片岩中挑选的锆石207Pb/206Pb年龄大部分位于1135±91Ma-1890±13Ma之间,少量年轻的锆石206Pb/238U年龄可以低至633±8Ma。结果表明宝音图群的原岩的沉积时代可以低至早古生代。侵入于宝音图群并随宝音图群一起变形变质的二长花岗岩的侵位年龄为446.4±1.OMa,变形变质年龄为399.4±1.5Ma,显示宝音图群的变形变质作用可能持续到早泥盆世。结合宝音图群主微量元素的分析显示,宝音图群的原岩应为沉积岩,其中角闪岩、斜长角闪岩可能为泥质、白云质沉积岩,二云石英片岩为石英含量不等的碎屑岩。二云石英片岩原岩的沉积环境可能为新元古代至古生代期间形成陆缘弧。
锆石SHRIMP U-Pb测年结果显示,早期黑云母二长花岗岩就位年龄约为273Ma,成矿期似斑状黑云母二长花岗岩就位年龄约为253Ma。矿区的岩浆活动构成了一个多阶段演化的,从早期逐渐增强至大规模岩浆上侵,随后衰减为小规模岩浆侵位,并伴随着大量成矿流体出溶的成矿岩浆活动周期。查干花斑岩钼矿化的发生是这个长期岩浆活动周期的结果。主微量元素和同位素研究显示,矿区内的两期花岗岩具有共同来源。主微量元素测试结果显示这两期花岗岩具有高度演化和分异的特征,是深部岩浆房内经历了一定程度结晶分异和同化混染的产物。这两期花岗岩也具有明显弧岩浆作用的特点,反映了深部岩浆源区可能受到了早期俯冲作用的改造,并在二叠纪期间的碰撞后伸展环境下就位。这两期花岗岩与兴蒙造山带内大量产出的新生的低(87Sr/86Sr)i高εNd(t)花岗岩具有明显的差异,(87Sr/86Sr)i变化范围较大,εNd(t)较低,显示上部地壳物质对岩浆的形成具有重要贡献,构成了成矿岩浆的地壳物质端元。同位素组成特征也显示受到了富集地幔EM1I的改造。
辉钼矿Re-Os同位素测年显示,斑岩钼矿化发生于～243Ma,晚于成矿期岩浆就位年龄近10Ma,是查干花成矿岩浆长期演化过程的反映,也与矿区地质特征相符。氢同位素组成具有明显的负值(δD可低至-133.9%0),硫同位素位于零值附近,但具有明显的正值(δ34S平均为2.97%0),显示成矿热液在岩浆中经历了明显的气液相瑞利分馏过程,也从侧面反映了成岩成矿过程的长期性。成矿期流体包裹体主要为气液两相H2O-NaCl体系,并含有少量的C02。测温结果显示,成矿期具有高均一温度(可高达387。C)和低盐度的特点。结合矿物对氧同位素温度计的研究结果,显示辉钼矿于653℃和200MPa (静岩压力深度7.4km)左右开始沉淀,并主要在384～416℃、40～65MPa(静水压力深度4-6.5km)环境下沉淀。矿床的形成与经历了明显去气作用的低盐度流体的长期演化有关,成矿流体气液相组分的分离是成矿系统内温度降低的重要原因,也是导致是辉钼矿沉淀的重要因素。矿床成矿期流体来源于岩浆,成矿物质的来源具有深部来源特征,可能来源于大陆下部岩石圈地幔及下地壳。
查干花矿床的地质特征和形成过程与伸展环境下高F型斑岩钼矿床具有明显的类似性,显示查干花斑岩钼矿床应属于高F型斑岩钼矿床。查干花也是兴蒙造山带内大型斑岩钼矿床(>10万吨)中最早形成者,其形成指示着兴蒙造山带内东西向-北东向大规模斑岩钼矿化的肇始。从查干花矿床的研究显示,晚古生代开始的碰撞后伸展构造环境及其控制下的高分异型岩浆活动对兴蒙造山带内大规模斑岩钼矿化的发生具有重要的贡献,但古生代期间的俯冲作用对矿床的形成同样具有重要意义。主要体现在以下几点：(1)塑造富集型岩浆源区.古生代期间的早期俯冲作用使得大陆岩石圈含有更高的地幔不相容元素(包括钼等成矿元素),进而构成成矿元素相对富集的大陆岩石圈；(2)水化造山带。早期的俯冲过程中的脱水熔融为兴蒙造山带输入了大量的水源,从而水化了造山带,为缺乏板块俯冲作用的碰撞后伸展环境中大规模斑岩钼矿化提供充足的成矿流体来源；(3)增厚大陆岩石圈。早期俯冲和碰撞过程使得兴蒙造山带形成加厚的大陆岩石圈,促进碰撞后伸展环境下岩石圈减薄,以及这个过程中的壳幔相互作用。
Located in Urat Rear Banner, Chaganhua is a typical and newly discovered large scale porphyry Mo deposit in Xing'an Mongolian orogenic belt. There are three main geological units occur in Chaganhua ore district:the Baoyintu Group metamorphic complex, the "X" shaped fractures and the Permian multistage intrusived granites. The Baoyintu Group metamorphic complex is medium-grade metamorphic rock and constitutes the main pre-ore basement. The Permian multistage intrusived granites is mainly composed of Early Permian biotite monzonitic granite and Late Permian porphyritic biotite monzonitic granite, the intrusion of later is controlled by the pre-ore "X" shaped fractures, and lead to the hydrothermal alteration and porphyry Mo mineralization of Chaganhua. The typical alteration includes potassic feldspathization, sericitization, silicification, argillization, epidotization and chloritization. The Mo mineralization is mainly hosted in porphyritic biotite monzonitic granite, and directly associated with the sericitization and silicification alteration. Most of the Mo mineralization occurs as vein and veinlet, based on the assemblage of alteration minerals of these vein and veinlet, they can divided into pre-mineralization quartz venlets, metallogenic quarzt-molybdnite-sericite venlets, quarzt-pyrite-sericite venlets, quarzt-molybdnite-venlets and quartz-wolframite vein and post-mineralization quartz-pyrite venlets.
LA-ICP-MS U-Pb dating study shows that most of zircons of plagioclase amphibolite from Baoyintu Group yield206Pb/238U ages ranging from464±5Ma to698±8Ma, and some of them yield207Pb/207Pb ages as old as1995±11Ma. Most of the zircons of two-mica quartz schist yield207Pb/207Pb ages ranging from1135±91Ma to1890±13Ma, and some of them yield206Pb/238U ages as young as633±8Ma. These ages show that the sedimentary time of the protolith of Baoyintu Group may as low as Middle Ordovician. The zircons from monzonitic granite which was deformated and metamorphic with Baoyintu Group yield two weighted mean concordant ages of446.4±1Ma and399.4±1.5Ma, these suggest that the monzonitic granite intruded the Baoyintu Group at Late Ordovician, and the time of metamorphism of Baoyintu Group may as low as Early Devonian. Incorporating the petrogeochemistry studies, we suggest that the protolithes of Baoyintu Group are sedimentary rocks, among which, the protolith of plagioclase amphibolite may be pelite mudstone, dolomite, and the protolith of two-mica quartz schist may be clastic rocks. These sedimentary may deposit in continental marginal arc formed in Late Proterozoic to Early Paleozoic.
SHRIMP U-Pb dating study shows that the pre-mineralization biotite monzonitic granite was emplaced at about273Ma, and the mineralization related porphyritic biotite monzonitic granite was emplaced at about273Ma.The emplacement of these granites constitute a long lived and multistaged magmatic evolution cycle, which was evolved from progressive magmatic activity to large-scale intrusion of granite, and waning to small-scale intrusion of ore forming magma, and to the exsolution of ore forming hydrothermal fluid. The mineralization activity is the outcome of this long lived magmatic evolution cycle. The petrogeochemistry studies suggest that these two granite intrusions share the same geochemical feature of highly evolved magma. We suggest that they are the consequence of AFC in the deep magma chamber under Chaganhua porphyry deposit, and their magma source was modified by the Paleozoic sudbuction of oceanic crust, and emplaced in Late Paleozoic extensional tectonic setting. The isotope chemistry studies show enriched feature for these granites, which are different from the low (87Sr/86Sr)i and high ε Nd(t) granites occurring Xing'an-Mongolia orogenic belt.We suggest that these granites are souced from two endmembers:upper crust and EMⅡ.
The molybdenite Re-Os dating show that the porphyry Mo mineralization occurred at about243Ma, which was about10Ma later than the emplacement of ore forming magma. This reflects a long duration of hydrothermal activity in Chaganhua deposit, which is agreed with the geological features of chaganhua deposit. These long duration are also supported by the stable isotopes studies, the ore forming fluid have very low δD (-133.9‰) and district positive δ34S (2.97‰), which show intense Rayleigh fractionation process of the ore forming fluid, and these also reflect a long evolution history of the ore forming fluid. Fluid inclusions in quartz of the main stage and late stage of molybdenum mineralization are mainly two phase vapor-liquid inclusions of H2O-NaCl composition with small amount of CO2phase. It's characterized by moderately low salinities and high homogenization temperatures. Combined with the studies of oxygen isotope thermometer, we suggest that molybdenum began to deposit at653℃,200MPa (approximately7.4km of lithostatic pressure) and mainly deposit at416℃to384℃,65MPa to40MPa (approximately6.5km to4km of hydrostatic pressure). The inclusions data combined with H-O isotope data record an evolution path of the hydrothermal fluid of degassed magma water source from high temperature, high pressure and moderately low salinity to low temperature, pressure and salinity which form Chaganhua porphyry molybdenum deposit, and these studies also suggest that the long fractionation history of ore foming fluid may be one of the important reasons for deposition of molybdnite. The H-O-S-Pb isotope geochemical studies also thow that the ore forming fluid are sourced from magmatic activity, and the ore forming substances are sourced from deep magma, and probably from subcontinental lithospheric mantle and lower crust.
The geology and metallogenic studies show that Chaganhua porphyry Mo deposit are comparable to the high F type porphyry Mo deposits occurs in extensional tectonic setting, and suggest Chaganhua is a high F type deposit. Chaganhua is also the oldest large scale porphyry Mo deposit occurring in Xing'an-Mongolia orogenic belt, its formation means the begining of extensive porphyry Mo mineralization along the S-E to NE trending Xing'an-Mongolia orogenic belt. The activity of highly evolved and differentiated magma in post-collision extensional setting may be of great significance, but the Paleozoic subduction-modified fertile magma source may also play a crucial role in the formation of these huge porphyry Mo mineralization belt as follows:(1) Building up the fertile magma source by subduction fluids enriched in incompatible elements in Paleozoic;(2) hydrating the orogenic belt by dehydration melting of subduction fluids in Paleozoic and this highly concentrated wate will be released in the post-collision extensional setting stage, and will contribute the huge volumes of ore forming fluid needed in the formation of this huge porphyry Mo mineralization belt in Xing'an-Mongolia orogenic belt;(3) Thickening the continental lithosphere in by subduction tectonism, the instability of this thickened lithosphere would thin again because of the termination of compressive stress in post-collision extensional setting, which will cause the extensive Crust-mantle interaction.
引文
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