新疆东准噶尔金水泉金矿床地质特征、成矿时代及其地质意义
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摘要
新疆奇台县金水泉金矿床是东准噶尔卡拉麦里成矿带上一个典型的造山型金矿床,产于清水-苏吉泉大断裂和卡拉麦里深断裂之间的次级断裂带中,其成矿时代尚无确切的年代学资料。通过阴极发光(CL)、背散射图像(BSE)和矿物包体确定含金石英脉中的锆石种类,进行LA-ICP-MS锆石U-Pb同位素定年。捕获锆石主要呈柱状、长柱状,振荡环带清晰,粒径较热液锆石大,包括岩浆锆石和变质锆石;~(206)Pb/~(238)U年龄为365~418Ma、265Ma。热液锆石呈短柱状、棱角状、不规则状、双锥状,常含继承锆石内核,内部包裹体为磷灰石或含金磷灰石,发育不明显的波缓状振荡环带或无振荡环带;~(206)Pb/~(238)U年龄加权平均值为314.9±3.2Ma,指示金矿化作用发生于晚石炭世早期碰撞造山向造山后伸展转变的构造环境。成矿时代晚于赋矿围岩姜巴斯套组的年龄(约343Ma),与总结区域构造演化规律所限定的时间范围(320~310Ma)吻合。综合研究认为,金水泉金矿床成矿作用可划分为350~320Ma造山阶段含金流体生成、315Ma挤压-伸展转换阶段金迁移就位、二叠纪陆内变形阶段金矿体破碎变形3个阶段。
Located in the Kalamaili metallogenic belt in the east Junggar of Xinjiang, the Jinshuiquan gold deposit is a typical orogenic gold deposit which occurs along the secondary fault zone between the Kalamaili deep fault and the major disruption of QingshuiSujiquan. The mineralization timing has been unclear up till now. Zircon species in auriferous quartz veins of this study were initially determined by cathodoluminescence electron(CL) images, Back Scattered Electron(BSE) image and mineral inclusions before the performance of LA-ICP-MS U-Pb isotopic dating on these zircons. The trapped zircons are mainly in the columnar and long columnar forms, with clear shock bands, consisting of magmatic zircons and metamorphic zircons. These zircons are larger than hydrothermal zircons. LA-ICP-MS U-Pb dating on these trapped zircons yielded ~(206)Pb/~(238)U ages of 365~418 Ma and 265 Ma. The hydrothermal zircons are in short columnar, angular, double cone and irregular forms and usually contain inclusions such as inherited zircon core, apatite or gold bearing apatite, some with weak band of shock waves or even without shock bands. LA-ICP-MS U-Pb dating on these hydrothermal zircons yielded a weighted average ~(206)Pb/~(238)U age of 314.9 ± 3.2 Ma, indicating that early Late Carboniferous gold mineralization occurred during the transition from collisional orogenesis to post-collisional extension. The metallogenic epoch was later the epoch of ore hosting wall rock, i.e., the Jiangbasitao Formation(C1 j, ~343 Ma) which coincides with the time frame(320~310 Ma) limited by the summarized orderliness of regional tectonic evolution from the data obtained by previous researchers. Comprehensive studies suggest that the metallogenic process of the Jinshuiquan gold deposit can be divided into three periods: the formation of gold bearing fluid at the orogenic stage during 350~320 Ma, the migration and emplacement of goldbearing hydrothermal fluid at 315 Ma during compression to extension stage and the fracture and deformation of gold orebody at the Permian intracontinental deformation stage.
Located in the Kalamaili metallogenic belt in the east Junggar of Xinjiang, the Jinshuiquan gold deposit is a typical orogenic gold deposit which occurs along the secondary fault zone between the Kalamaili deep fault and the major disruption of QingshuiSujiquan. The mineralization timing has been unclear up till now. Zircon species in auriferous quartz veins of this study were initially determined by cathodoluminescence electron(CL) images, Back Scattered Electron(BSE) image and mineral inclusions before the performance of LA-ICP-MS U-Pb isotopic dating on these zircons. The trapped zircons are mainly in the columnar and long columnar forms, with clear shock bands, consisting of magmatic zircons and metamorphic zircons. These zircons are larger than hydrothermal zircons. LA-ICP-MS U-Pb dating on these trapped zircons yielded ~(206)Pb/~(238)U ages of 365~418 Ma and 265 Ma. The hydrothermal zircons are in short columnar, angular, double cone and irregular forms and usually contain inclusions such as inherited zircon core, apatite or gold bearing apatite, some with weak band of shock waves or even without shock bands. LA-ICP-MS U-Pb dating on these hydrothermal zircons yielded a weighted average ~(206)Pb/~(238)U age of 314.9 ± 3.2 Ma, indicating that early Late Carboniferous gold mineralization occurred during the transition from collisional orogenesis to post-collisional extension. The metallogenic epoch was later the epoch of ore hosting wall rock, i.e., the Jiangbasitao Formation(C1 j, ~343 Ma) which coincides with the time frame(320~310 Ma) limited by the summarized orderliness of regional tectonic evolution from the data obtained by previous researchers. Comprehensive studies suggest that the metallogenic process of the Jinshuiquan gold deposit can be divided into three periods: the formation of gold bearing fluid at the orogenic stage during 350~320 Ma, the migration and emplacement of goldbearing hydrothermal fluid at 315 Ma during compression to extension stage and the fracture and deformation of gold orebody at the Permian intracontinental deformation stage.
引文
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[14]Kerrich R, King R W. Hydrothermal zircon and baddeleyite in Val-d’Or Archean mesothermal gold deposits:Characteristics,compositions, and fluid-inclusion properties, with implications for timing of primary gold mineralization[J].Can. J. Earth Sci., 1993,30:2334-2351.
[15]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.
[16]顾雪祥,董连惠,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.
[17]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.
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[20]宋利宏,朱光,顾承串,等.卡拉麦里断裂带造山期活动规律及其对造山过程的指示[J].地质论评, 2015, 1:8.
[21]Liu Y S, Hu Z C, Zong K Q, et al. Reappraisement and refinement of zircon U-Pb isotope and traceelement analyses by LA-ICP-MS[J]. Chinese Science Bulletin, 2010, 55(15):1535-1546.
[22]李长民.锆石成因矿物学与锆石微区定年综述[J].地质调查与研究, 2009, 32(3):161-174.
[23]吴元保,郑永飞.锆石成因矿物学研究及其对U-Pb年龄解释的制约[J].科学通报, 2004, 49(16):1589-1604.
[24]张永清,王国明,许雅雯,等.锆石微区原位U-Pb定年的测定位置选择方法[J].地质调查与研究, 2015, 38(3):233-238.
[25]吴琪,屈迅,常国虎,等.红柳峡韧性剪切带形成时代及其对准噶尔洋盆闭合时限的约束[J].岩石学报, 2012, 28(8):2331-2339.
[26]黄岗,牛广智,王新录,等.新疆东准噶尔卡拉麦里蛇绿岩的形成和侵位时限——来自辉绿岩和凝灰岩LA-ICP-MS锆石UPb年龄的证据[J].地质通报, 2012, 31(8):1267-1278.
[27]唐红峰,苏玉平,刘丛强,等.新疆北部卡拉麦里斜长花岗岩的锆石U-Pb年龄及其构造意义[J].大地构造与成矿学, 2007, 31(1):110-117.
[28]李锦轶.新疆东部新元古代晚期和古生代构造格局及其演变[J].地质评论, 2004, 50(3):304-322.
[29]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.
[30]方爱民,王世刚,张俊敏,等.新疆北部卡拉麦里蛇绿岩中辉长岩的锆石U-Pb年龄及其构造意义[J].地质科学, 2015, 50(1):140-154.
[31]赵恒乐,许凡,张冀,等.东准噶尔卡拉麦里蛇绿岩形成时代、地质特征及构造意义[J].新疆地质, 2012, 30(2):161-164.
[32]赵玉锁,路彦明,马德锡.东准卡拉麦里地区放射虫硅质岩地球化学特征[J].西北地质, 2008, 41(3):64-70.
[33]樊立飞,赵斌斌,代俊峰,等.新疆东准噶尔卡拉麦里蛇绿岩带研究现状[J].甘肃地质, 2014, 23(2):21-26.
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