西准噶尔宝贝金矿区小岩株锆石U-Pb年代学及其对成矿的时代制约

王乐民，段丰浩，纪征宝，王冉，赵得龙，郭鑫，程万里

(1.新疆维吾尔自治区国土资源厅,新疆 乌鲁木齐 830002；2.长安大学地球科学与资源学院，陕西 西安 710054；3.新疆地质矿产勘查开发局第七地质大队，新疆 乌苏 833000)

西准噶尔宝贝金矿区小岩株锆石U-Pb年代学及其对成矿的时代制约

王乐民1，段丰浩2，纪征宝3，王冉2，赵得龙2，郭鑫2，程万里2

(1.新疆维吾尔自治区国土资源厅,新疆 乌鲁木齐 830002；2.长安大学地球科学与资源学院，陕西 西安 710054；3.新疆地质矿产勘查开发局第七地质大队，新疆 乌苏 833000)

宝贝金矿区出露面积较小的二长花岗岩体，其对该区金矿的成矿作用贡献如何是重要的地质问题。为此，笔者进行了该岩体的年代学工作。为区域金矿的成矿时代提供精确的同位素年代学约束。该矿床硫化物组合单一，主要为黄铜矿。笔者选择了1件样品，进行LA-ICPMS锆石U-Pb法定年。结果10个测点给出的等时线年龄为(300.3±8.6)Ma。这表明该区Au的成矿作用有可能是由该区晚石炭世—早二叠世的大规模岩浆活动来提供物质来源和热动力条件等，具有十分重要的成矿意义。

宝贝金矿；LA-ICP-MS锆石U-Pb定年；区域成矿；西准噶尔

西准噶尔地区已发现较多的金矿床，尤其在达尔布特断裂带北侧较为集中。该带晚古生代岩浆活动强烈，火山岩和侵入岩广布，峰期为石炭纪—早二叠世(韩宝福等，2006, 苏玉平等，2006, Tang, et al., 2010, Yin, et al., 2010, 魏少妮等，2011, 尹继元等，2011)。该带Cu-Mo-W-Be等成矿元素组合好，异常有一定规模分布(陈宣华等，2015)，西准噶尔地区发育还原性斑岩铜矿和石英脉型-斑岩型钨钼矿，具有Cu-Au-Mo-W组合(Shen, et al., 2013)。前人对该区金矿和岩浆活动的关系有一定认识。从成岩时代上看，碱性花岗岩类时代集中在308～296Ma之间(苏玉平，2006, 韩宝福，2006, Geng, et al., 2009, 冯乾文等，2012)。对于钙碱性的中酸性小岩体而言，包古图一带小岩体的年代学资料较多，主要集中在313～319Ma之间(张连昌等，2006, 宋会侠，2007, 宋会侠等，2007, Song, et al., 2007, 郑波等，2009, Liu, et al., 2009, Shen, et al., 2009, 魏少妮等，2010, Shen, et al., 2010, Shen, et al., 2010, Tang, et al., 2010, 魏少妮，2011, Shen, et al., 2012, Tang, et al., 2012, Shen, et al., 2013, 郑波等，2014)。统计意义上看，区域上与Cu-Mo的成矿可能与钙碱性系列的中酸性小岩体有关，尤其是斑岩型矿床(点)(张连昌，2006, Liu, et al., 2009, Tang, 2010, 李永军等，2012, Wang, et al., 2013, 鄢瑜宏等，2014, 鄢瑜宏等，2015, 申萍等，2015)。

然而，区域金矿的成矿地质背景尚需进一步探讨，缺乏与区域岩浆活动关系的探讨(陈衍景，1996)。宝贝金矿是其中一个较大金矿，该矿床与区域岩浆活动有何关系也未得到深入的研究。要解决这一问题，年代学工作十分必要。笔者为此而展开矿区二长花岗岩的锆石U-Pb法定年工作，探讨矿区岩浆活动的时代。这为金矿的形成背景提供了重要年代学制约。

1 区域地质

西准噶尔构造带位于中亚造山带西南部，是中亚古生代俯冲-增生复合造山带的主要组成部分(Feng, et al., 1989, 肖序常等，1992, 何国琦，2004, 李锦轶等，2006, Xiao, et al., 2009, 李锦轶等，2009, Wilhem, et al., 2012, Choulet, et al., 2013, Zhu, et al., 2013)，发育多条蛇绿(混杂)岩带(Zhang, et al., 2011, Yang, et al., 2013, Zhu, 2013)和大量中酸性侵入岩(图1)。NE向的达尔布特断裂带两侧侵入岩尤其发育，包括夏尔莆(克拉玛依)、红山、铁厂沟、阿克巴斯陶等大岩基以及包古图、别鲁阿嘎希、玉依塔勒盆克提等小岩体(金成伟等，1993)，构成了著名的达尔布特构造岩浆带和具有找矿潜力的岩浆成矿带(李永军，2012)。该带地层主要为泥盆纪—石炭纪陆源碎屑岩-火山碎屑岩建造，见有火山岩夹层，火山岩时代为(328.1±1.8)Ma～(357.5±5.4)Ma(王瑞等，2007, 安芳等，2009, 佟丽莉等，2009)。

宝贝一带的二长花岗岩体侵入于早石炭世地层中(图2)。断层发育，矿化体赋存于岩体围岩中，部分为石英脉型矿化，石英脉和断层带中矿化特征明显。该岩体出露面积有限，地表显示为哑铃状。位于西准噶尔的宝贝金矿主要由石英脉型矿石组成，主要含金矿物为银金矿，以裂隙金和包裹金的形式赋存在毒砂、黄铁矿和石英中(王瑞，2007)。

2 样品和分析方法

用于锆石LA-ICP-MS U-Pb测年的样品采自岩体近中心，样品编号BBRZ-1。采样位置利用GPS定位，经纬度为：45°54'17.87"北，84°38'35.17"东，海拔为961m(图2)。

样品岩性为浅肉红色细粒二长花岗岩，未见包体。岩体周围见有大量含金石英脉。岩石由斜长石、钾长石、石英组成，含少量黑云母。斜长石约占40%：呈半自形板状，粒径0.2～1.0mm，可见聚片双晶，轻度绢云母化、泥化。钾长石约占30%：他形粒状，粒径0.3～1.4mm，具条纹结构，为条纹长石，轻度泥化。石英约占30%：他形粒状，粒径0.2～1.6mm，波状消光，分布不均匀。黑云母少量：片状，片径0.1～0.4mm，黄-褐色。磁铁矿微量：粒状，粒径0.1～0.2mm。

JFS.加甫萨尔苏;XEP.夏尔莆;BGT.包古图;HS.红山;TCG.铁厂沟;HT.哈图;AKB.阿克巴斯套;MEG.庙尔沟;TEG.塔尔根;DLNL.多拉那勒;YGZ.也格孜卡拉;HGLL.洪古勒楞;N.TC.塔城北;TST.托斯特;KWSY.孔吾萨伊;KSB.卡桑布拉克;KYTS.阔依塔斯;KEJ.卡尔交;KLMS.库鲁木苏;SLK.赛力克;TLG.托洛盖;AL.宝贝金矿区;BL.别鲁阿嘎希;YY.玉依塔勒盆克提;HLZ.黄梁子;GETS.加尔塔斯;LB.拉巴;DLH.都伦河东;TS.塔斯阔腊; BE.布尔科斯台;KZ.克孜勒巴斯陶;JW.吉乌尔沙克;AL.阿拉散布拉克;K1.克I岩体;K2.克II岩 体;HSD.红山东岩体;SETH.萨尔托海岩株;BB.宝贝二长花岗岩体图1 西准噶尔地质简图及Au、Cu、Mo矿点(化)(改自新疆维吾尔自治区地质矿产局, 1993，ChenJ, et al., 2010,ChenJ, et al., 2014)Fig.1 Geological map of the West Junggar region with the location of Au-Cu-Mo deposit occurrences (Modified from XJBGME, 1993;Chen J, et al., 2010; Chen J, et al., 2014)

锆石分选在廊坊诚信地质服务有限公司完成，样品重量约5kg。样品人工破碎并使用可清洗分选设备淘洗和富集重矿物，后以磁选和电磁选获非电磁性矿物，再行淘洗富集锆石，最后在双目镜下手工挑选锆石。

将待测锆石以环氧树脂固定，抛光至暴露出锆石中心面，用反射光、透射光照相。然后用体积百分比为3%的HNO3清洗样品并镀碳，进行阴极发光(CL)照相。照相之后用3%的HNO3清洗靶标的表面。

激光剥蚀电感耦合等离子体质谱(LA-ICP-MS)原位U-Pb 定年在西北大学大陆动力学国家重点实验室完成。实验采用的ICPMS 为美国Agilent 公司生产的Agilent 7500 a，激光剥蚀系统为德国MicroLas公司生产的GeoLas 200 M，该系统由德国Lambda Physik 公司的ComPex102 ArF 准分子激光器(波长193 nm)与MicroLas 公司的光学系统组成。激光剥蚀束斑直径约为30μm，激光剥蚀样品的深度为20～40 μm。详细分析步骤和数据处理方法参见参考文献(Yuan, et al., 2008)。用LA-ICP-MS Common Lead Correction(v. 3.15)对其进行了普通铅校正(Andersen, 2002)，使用Isoplot软件计算U-Pb年龄(Ludwig, et al., 1991)。

图2 (a)宝贝金矿一带二长花岗岩锆石U-Pb谐和图和(b)年龄直方图及代表性锆石的 阴极发光图像(小插图)Fig.2 (a) LA-ICPMS U-Pb Concordia plots and (b)statistical histograms of U-Pb dating for zircons from the Baobei pluton. The insert picture showing representatives of Cathodoluminescence image of zircons from monzonitic granite in Baobei area.

3 分析结果

本次自未有明显蚀变的样品BBRZ1中获得的锆石为棱柱状，CL图像显示其为典型的岩浆锆石(图2中小插图)，具有明显的环带状结构。锆石U-Pb分析结果列于表1，其中17个测点由于206Pb/238U和207Pb/235U年龄不谐和(图2b)，为离群点，没有参与计算。RZ-23、24两个测点年龄偏老，没有参与计算。这类误差较大的数据表面年龄集中在晚石炭世至早二叠世，有可能遭受了热液的改造造成U-Pb体系的破坏以及Pb的丢失。

其余有效测点年龄数据总计10个，206Pb/238U加权平均年龄为(300.3±8.6)Ma(2σ)(图2b)，代表了岩浆结晶的时代。该年龄十分接近于红山等A2型花岗岩体(韩宝福，2006, 苏玉平，2006)，而明显晚于包古图一带的小岩体(Tang, 2010)。

4 讨论与结论

4.1 成岩成矿时代

区域重要矿点的成矿年代学已有数据积累。宏远斑岩体辉钼矿的Re-Os等时线年龄为 294.6±4.6 Ma之间(Wang, 2013)，但也有(314.3±1.9)Ma(鄢瑜宏，2014)的可能。包古图一带的辉钼矿的Re-Os 年龄将成矿年龄限定在(310±6.4)～(316 ±6.4)Ma(宋会侠，2007, 申萍等，2010)。该岩体侵入于早石炭世地层中，也证实其是在晚石炭世之后侵位的。铜矿脉空间上赋存于夏尔浦岩体靠北的花岗闪长岩中。该岩体的时代也有较多锆石U-Pb年代学数据，其中的花岗岩体、辉绿岩脉和花岗岩脉时限为301～321Ma(Kwon, et al., 1989, 韩宝福，2006, 贺敬博等，2011)。本研究的结果(300.3±8.6)Ma与之非常接近而略晚，表明成矿流体可能来自于岩浆热液或者成矿热源来自岩浆。

按照前人对该区成矿区带规律的研究，区内的金等矿床主要就位于晚石炭世—二叠纪,集中分布在碰撞造山作用较强烈的地带,矿床形成于碰撞作用的挤压-伸展转变期(陈衍景，1996)。

4.2 宝贝金矿与区域岩浆活动的关系及成矿意义

中亚造山带是世界上最大的增生型造山带，造就了巨量金属堆积，形成了中亚成矿域(Seng, et al., 1993, Jahn, et al., 2004, Windley, et al., 2007, Pirajno, et al., 2008, Wilhem, 2012)。西准噶尔地体位于中亚造山带西南一带，且石炭纪-早二叠世是新疆北部最为重要的金属矿床成矿期(Yakubchuk, 2004, Seltmann, et al., 2005, 肖文交等，2006, 朱永峰等，2007, 冯京等，2010, 杨富全等，2010, 尹继元，2011)。西准噶尔南部尤其是达尔布特断裂带两侧，侵入岩分布广泛，可分为小岩体、大岩基和中基性岩墙或者岩脉(沈远超等，1993)。小岩体包括包古图的Ⅰ至Ⅹ号(如魏少妮等, 2015)、加尔塔斯(刘建平等，2009)、玉依塔勒盆克提(Zhang, et al., 2015)等小岩体，均与Cu-Au矿床或矿化有关，这些小岩体岩性主要为石英闪长岩和花岗闪长岩。大岩基包括如哈图、铁厂沟、庙儿沟、阿克巴斯套、加甫沙尔苏、红山，这些大岩基大部分没有Cu-Au矿化，大多数为A2型花岗岩(苏玉平，2006)。大岩基的年代学研究较为深入，时代集中在308～296Ma之间(苏玉平，2006, 韩宝福，2006, Geng, 2009, 冯乾文，2012)。小岩体的研究工作主要集中在包古图一带，时代主要集中在313～319Ma，具有埃达克型岩石的地球化学特征(张连昌，2006, Song, 2007, Shen, 2009, Tang, 2010, Shen, 2012)。但是，同时一些二长花岗岩和正长花岗岩往往出露面积也较小，周围发育大量石英脉，往往产有Au矿床。

统计意义上讲，区域上大多数Cu-Au矿与晚古生代岩浆作用有关。该带Cu-Mo-W-Be等成矿元素组合好，异常有一定规模分布(陈宣华，2015)，西准噶尔地区发育还原性斑岩铜矿和石英脉型-斑岩型钨钼矿，具有Cu-Au-Mo-W组合(Shen, 2013)。此外，以前该区的成矿时代主要集中在晚石炭世早期如包古图等(Song, 2007, Liu, 2009, Shen, 2009, Shen, 2012)。根据环形影像特征、色调差异及环形水系特征，该区还识别出了不同尺度的岩体和(或)隐伏岩体(魏永明等，2015)，也说明西准噶尔地区成矿地质条件不仅优越，而且有待进一步深入研究。

综上所述，本次早二叠世早期的年代学资料证实该区可能存在晚石炭世—早二叠世的成矿作用，有可能是由该期大规模的A2型花岗质岩浆作用供给成矿物质来源和热动力的。

致谢:野外地质工作得到了新疆地矿局第七地质大队同行的大力帮助。长安大学李永军教授在野外调研、论文写作及分析测试工作中给予了帮助和指导。

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Zircon U-Pb Geochronology of Pluton from Baobei Gold Orefield in Western Junggar and Its Metallogenic Significance

WANG Lemin1, DUAN Fenghao2, JI Zhengbao3, WANG Ran2, ZHAO Delong2,GUO Xin2, CHENG Wanli2

(1. Xinjiang Department of Land and Resources; Urumqi 830002, Xinjiang , China; 2. Earth Science & Resources College of Chang’an University, Xi’an 710054, Shaanxi, China; 3. No.7 Geological Party，Xinjiang Bureau of Geology and Mineral Resources Exploration, Wusu 833000, Xinjiang, China)

The Baobei Au deposit is located in the West Junggar region of Xinjiang. The pluton has been found in the deposit area that intruded into Early Carboniferous sedimentary strata. U-Pb dating for samples obtained from the granite in the deposit yield a weighted mean age of (300.3 ± 8.6) Ma (2, N=10), which is consistent with the peak ages of the magmatic activity in the West Junggar region, indicating that the deposit is genetically related with an early Permian metallogenic system. This consistency suggests the relative large potentiality of finding more Cu deposits in the belt.

Baobei gold deposit; LA-ICP-MS zircon U-Pb dating; regional metallogenisis; west Junggar

2015-04-01；

2015-05-07

国家自然科学基金项目(41402044)、中国博士后基金特别资助项目(2013T60869)和新疆两权中央留成专项资金项目(Y14-5-LQ06)联合资助

王乐民(1971-),男,甘肃永登人, 本科，1997年毕业于东华理工大学地质矿产勘查专业，高级工程师。E-mail：WLM66888@163.com

P618.51

A

1009-6248(2015)03-0241-10