新疆东准噶尔南明水金矿床成矿流体特征:流体包裹体及氢氧同位素证据
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摘要
新疆东准噶尔南明水金矿床位于卡拉麦里成矿带东段,矿体受NW—NWW向韧-脆性断裂控制,赋矿围岩为下石炭统姜巴斯套组的浅变质海相火山碎屑-沉积岩。以流体包裹体和氢、氧同位素为研究手段,查明了矿床成矿流体性质、来源及其演化特征与金成矿的关系。其热液成矿过程可划分早、中、晚3个阶段,石英中原生包裹体主要有CO_2-H_2O包裹体、水溶液包裹体和纯CO_2包裹体3种类型。早阶段石英中以CO_2-H_2O包裹体和纯CO_2包裹体为主,均一温度变化于257～339℃,盐度为0. 4%～2. 2%;中阶段石英中3种类型包裹体均发育,CO_2-H_2O包裹体和水溶液包裹体均一温度为196～361℃,盐度为0. 4%～6. 0%;晚阶段石英中仅见水溶液包裹体,均一温度相对较低,为174～252℃,盐度为1. 4%～3. 2%。由CO_2-H_2O包裹体计算的早、中阶段捕获压力分别为214～371 MPa、236～397MPa,对应的成矿深度分别为8. 1～14. 0 km、8. 9～15. 0 km。成矿流体由早、中阶段的CO_2-H_2O-NaCl±CH_4体系演化至晚阶段贫CO_2的H_2O-NaCl体系,成矿温度和流体密度呈逐渐降低趋势,盐度变化不大。流体包裹体和氢、氧同位素研究表明,主成矿阶段成矿流体主要来源于变质水,CO_2-H_2O-NaCl流体的不混溶是导致Au富集成矿的重要机制,南明水金矿属于中深成造山型金矿床。
The Nanmingshui gold deposit is located in the eastern part of the Kalamaili metallogenic belt. Its ore-bodies,controlled by the NW—NWW trending ductile-brittle faults,are hosted in epimetamorphic marine volcaniclastic sedimentary rocks of the Lower Carboniferous Jiangbasitao Formation. Based on the studies of fluid inclusions and hydrogen and oxygen isotopic geochemistry,the properties,source and evolution of ore-forming fluids are discussed in this paper. The ore-forming process can be divided into three metallogenic stages including the early,middle and late stages. Three types of fluid inclusions that include CO_2-H_2O,H_2O-NaCl and pure CO_2 inclusions are identified in the quartz of the Nanmingshui gold deposit. The early-stage quartz mainly contains CO_2-H_2O and pure CO_2 inclusions with homogenization temperatures and salinities ranging from 257 ℃to 339 ℃ and 0. 4% to 2. 2%. All three types of inclusions are trapped in the middle( main)-stage quartz. The homogenization temperatures and salinities of CO_2-H_2O and H_2O-NaCl inclusions vary from 196 ℃ to 361 ℃and 0. 4% to 6. 0%. Only H_2O-NaCl inclusions are found in the late stage quartz with relatively lower homogenization temperatures clustering at 174 ℃ to 252 ℃. Meanwhile,the salinities of H_2O-NaCl inclusions vary from 1. 4% to 3. 2%. According to the estimation from CO_2-H_2O inclusions,the minimum trapping pressures for early and middle stages are 214 MPa to 371 MPa and 236 MPa to 397 MPa,respectively,corresponding to the metallogenic depths of 8. 1 km to 14. 0 km and 8. 9 km to 15. 0 km,respectively. The studies of fluid inclusions in different metallogenic stages indicate that the metallogenetic temperatures and fluid densities show a decreasing trend,as the ore-forming fluids are evolved from CO_2-H_2O-NaCl ± CH_4 system in the early and middle stages to H_2O-NaCl system in the late stage. Fluid inclusions and hydrogen and oxygen isotopic studies show that the ore-forming fluids of the main metallogenic stage were dominantly originated from metamorphic water.The immiscibility of CO_2-H_2O-NaCl fluids is an important mechanism that leads to the gold precipitation and enrichment. The genesis of the Nanmingshui gold deposit is a mesozonal to hypozonal orogenic gold deposit.
The Nanmingshui gold deposit is located in the eastern part of the Kalamaili metallogenic belt. Its ore-bodies,controlled by the NW—NWW trending ductile-brittle faults,are hosted in epimetamorphic marine volcaniclastic sedimentary rocks of the Lower Carboniferous Jiangbasitao Formation. Based on the studies of fluid inclusions and hydrogen and oxygen isotopic geochemistry,the properties,source and evolution of ore-forming fluids are discussed in this paper. The ore-forming process can be divided into three metallogenic stages including the early,middle and late stages. Three types of fluid inclusions that include CO_2-H_2O,H_2O-NaCl and pure CO_2 inclusions are identified in the quartz of the Nanmingshui gold deposit. The early-stage quartz mainly contains CO_2-H_2O and pure CO_2 inclusions with homogenization temperatures and salinities ranging from 257 ℃to 339 ℃ and 0. 4% to 2. 2%. All three types of inclusions are trapped in the middle( main)-stage quartz. The homogenization temperatures and salinities of CO_2-H_2O and H_2O-NaCl inclusions vary from 196 ℃ to 361 ℃and 0. 4% to 6. 0%. Only H_2O-NaCl inclusions are found in the late stage quartz with relatively lower homogenization temperatures clustering at 174 ℃ to 252 ℃. Meanwhile,the salinities of H_2O-NaCl inclusions vary from 1. 4% to 3. 2%. According to the estimation from CO_2-H_2O inclusions,the minimum trapping pressures for early and middle stages are 214 MPa to 371 MPa and 236 MPa to 397 MPa,respectively,corresponding to the metallogenic depths of 8. 1 km to 14. 0 km and 8. 9 km to 15. 0 km,respectively. The studies of fluid inclusions in different metallogenic stages indicate that the metallogenetic temperatures and fluid densities show a decreasing trend,as the ore-forming fluids are evolved from CO_2-H_2O-NaCl ± CH_4 system in the early and middle stages to H_2O-NaCl system in the late stage. Fluid inclusions and hydrogen and oxygen isotopic studies show that the ore-forming fluids of the main metallogenic stage were dominantly originated from metamorphic water.The immiscibility of CO_2-H_2O-NaCl fluids is an important mechanism that leads to the gold precipitation and enrichment. The genesis of the Nanmingshui gold deposit is a mesozonal to hypozonal orogenic gold deposit.
引文
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(1)武警黄金第八支队.新疆东准噶尔地区构造-岩浆作用与多金属成矿关系调查报告(内部资料). 2017.
[2]张栋,路彦明,葛良胜,等.东准噶尔卡拉麦里地区金铜多金属成矿系统和地球动力学[J].地质论评,2015,61(4):797-816.
[3]程海伟.新疆卡拉麦里成矿带金矿床地质特征及其时空分布[J].新疆有色金属,2014,37(增刊):42-44.
[4]闫晓兰,李逸凡,刘红涛.新疆卡拉麦里造山型金矿系统[J].新疆地质,2014,32(3):328-333.
[5]杨富全,吴海.新疆东准噶尔金矿成因类型及地质特征[J].地质找矿论丛,2000,15(1):39-45.
[6]郭全,薄科武,赵军.新疆卡拉麦里山变质碎屑岩型金矿成矿条件分析[J].西部探矿工程,2007,19(10):164-167.
[7]路彦明,张栋,范俊杰,等.新疆东准地区成岩、成矿与构造演化时空耦合[J].矿床地质,2008,27(增刊):33-41.
[8]徐斌.新疆卡拉麦里成矿带金矿构造—岩浆控矿规律及找矿预测研究[D].北京:中国地质大学(北京),2010:30-48.
[9]聂晓勇,宋谢炎,章文忠,等.新疆东准地区卡拉麦里蛇绿岩带中两类金矿床的可能成因[J].矿床地质,2010,29(增刊):84-91.
[10]李锦轶,肖序常,汤耀庆,等.新疆东准噶尔卡拉麦里地区晚古生代板块构造的基本特征[J].地质论评,1990,36(4):305-316.
[11]蔡土赐.新疆维吾尔自治区岩石地层[M].武汉:中国地质大学出版社,1999:54-61.
[12]顾雪祥,董连慧,王新利,等.西天山博罗科努铜钼多金属成矿系统与靶区评价[M].北京:地质出版社,2017:1-4.
[13]赵磊,季建清,徐芹芹,等.新疆北部卡拉麦里晚古生代走滑构造及其叠加变形序次[J].岩石学报,2012,28(7):2257-2268.
[14]李锦轶.新疆东准噶尔蛇绿岩的基本特征和侵位历史[J].岩石学报,1995,11(增刊):73-84.
[15]李锦轶,杨天南,李亚萍,等.东准噶尔卡拉麦里断裂带的地质特征及其对中亚地区晚古生代洋陆格局重建的约束[J].地质通报,2009,28(12):1817-1826.
[16]张玉杰,张栋,路彦明,等.新疆东准噶尔卡拉麦里构造带多期变形和金叠加成矿[J].地质与勘探,2013,49(5):797-812.
[17]张守林,杨自安,傅水兴.新疆卡拉麦里成矿带赋矿岩层-矿化蚀变遥感特征[J].地质与勘探,2001,37(5):41-44.
[18]董静.新疆卡拉麦里清水泉金铜矿床地球化学特征及成因研究[D].乌鲁木齐:新疆大学,2015:9-13.
[19]徐春华,纪瑞元,郭文杰,等.韧性剪切带中金成矿地质构造解析方法及找矿预测——以卡拉麦里大断裂带金矿为例[J].河南科学,2015,33(7):1199-1205.
[20] CLAYTON R N,MAYEDA T K. The use of bromine pentafluoride in the extraction of oxygen from oxides and silicates for isotopic analysis[J]. Geochimica et Cosmochimica Acta,1963,27(1):43-52.
[21] COLEMAN M L,SHEPHERD T J,DURHAM J J,et al. Reduction of water with zinc for hydrogen isotope analysis[J]. Analytical Chemistry,1982,54(6):993-995.
[22] HALL D L,STERNER S M,BODNAR R J. Freezing point depression of Na Cl-KCl-H2O solutions[J]. Economic Geology,1988,83(1):197-202.
[23]刘斌,段光贤. Na Cl-H2O溶液包裹体的密度式和等容式及其应用[J].矿物学报,1987,7(4):345-352.
[24] ROEDDER E. Fluid Inclusions:Reviews in Mineralogy[M].Washington:Mineralogical Society of America,1984:1-644.
[25] SHEPHERD T J,RANKIN A H,ALDERTON D H M. A Practical Guide to Fluid Inclusion Studies[M]. Blackie:Chapman Hall,1985:1-239.
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