2016, Vol. 32
2. 中国地质科学院矿产资源研究所, 国土资源部成矿作用与资源评价重点实验室, 北京 100037 ;
3. 广西壮族自治区区域地质调查研究院, 桂林 541003
2. MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China ;
3. Institute of Regional Geological Survey of Guangxi Zhuang Autonomous Region, Guilin 541003, China
卡林型金矿是一种沉积岩容矿的微细浸染型金矿床，在全球该类型矿床主要分布于美国内华达州北部地区和我国的右江盆地及西秦岭地区(Hu et al., 2002；Zhang et al., 2003；Cline et al., 2005；Kesler et al., 2005; Peters et al., 2007；Su et al., 2008, 2009a, 2012；Hu and Zhou, 2012)。近年来的研究表明，美国内华达的卡林型金矿主要形成于33~42Ma(Tretbar et al., 2000；Cline, 2001；Arehart et al., 2003)，与区内始新世大规模岩浆活动具有一定的成因联系(Henry and Boden, 1998；Ressel et al., 2000；Ressel and Henry, 2006；Muntean et al., 2011；Johnson et al., 2015)。我国右江盆地发育的卡林型金矿与美国内华达州具有很多相似性，但其形成时代和成矿机理(包括硫、金及成矿流体的来源等)却远未得到有效约束。成矿时代方面，前人针对各类矿物采用了多种定年方法，给出了十分宽泛的年龄范围：36~267Ma(Hu et al., 2002；胡瑞忠等，2007a；Su et al., 2009b；Chen et al., 2015)。其中，如下两组年龄可能相对集中：(1) 通过方解石Sm-Nd同位素定年，获得了数个卡林型金矿的成矿时代可能为135~150Ma(Su et al., 2009b；王泽鹏，2013)；(2) 含砷黄铁矿、毒砂Re-Os及云母40Ar/39Ar和蚀变成因金红石U-Pb定年结果表明，金成矿时代可能为200~230Ma左右(陈懋弘等, 2007, 2009；Chen et al., 2015)。成矿机理方面，不少学者提出岩浆作用对金成矿十分关键(黄永全和崔永勤，2001；刘建中等，2006；王泽鹏，2013)。然而，除与峨眉山地幔柱有关的基性侵入体外(260Ma；Xu et al., 2008)，右江盆地内部火成岩出露十分有限；现有的研究表明，区内发育的少量超基性和酸性脉岩主要形成于80~100Ma(Liu et al., 2010c；陈懋弘等, 2012, 2014)，较上述两组成矿年龄明显年轻，且部分矿区发现脉岩切穿金矿体的地质现象(陈懋弘等，2014)。因而，很难将卡林型金矿与已出露的岩浆活动联系起来。然而，就区内是否存在隐伏岩体及其与金成矿是否存在成因联系等科学问题，目前尚不明确。
作者的初步研究显示，上述晚白垩世酸性脉岩往往富含大量的继承锆石。尽管继承锆石的来源十分复杂，但依然可能为早期的、隐伏的岩浆活动带来一些指示(Hoskin and Schaltegger, 2003；Pereira et al., 2011)。因而，对这些继承锆石进行深入研究，可能会为我们评估岩浆作用对金成矿的贡献提供有益的线索。本文选取右江盆地出露的三处酸性脉岩(其中两处与金矿床具紧密的空间联系)中的继承锆石为研究对象，通过锆石U-Pb定年手段，提取区内隐伏的岩浆岩信息并分析其构造意义，进而探究岩浆活动与卡林型金矿是否存在成因联系。
2 地质背景右江盆地位于扬子克拉通(其与华夏陆块共同组成华南板块)的西南缘，并以哀牢山-红河断裂与西南侧的三江古特提斯构造域相连(图 1；Peters et al., 2007；Hu and Zhou, 2012)。盆地南侧与越北陆块为邻，二者可能被另一条古特提斯洋缝合带(即滇琼缝合带，图 1a，Cai and Zhang, 2009；Yang et al., 2012a)隔开。连同师宗-弥勒断裂、凭祥-南宁断裂和紫云-亚都断裂，右江盆地被限制在一个近三角形的区域，故该区又被成为滇黔桂“金三角”。一般认为，早古生代晚期，伴随着古特提斯洋的打开，本区发生裂解并形成裂谷盆地，同时接受了大量浅水相的碳酸盐岩沉积(Liu et al., 2002；杜远生等，2013)。至中三叠世，由于古特提斯洋的闭合，该区演变为前陆盆地，并发育以砂岩和泥岩为代表的深水浊流相沉积(Enos et al., 2006)。详细的镜下鉴定表明，该套沉积岩中含有大量的火山碎屑物质(Yang et al., 2012b)。值得指出的是，盆地西北侧发育中三叠世碳酸盐岩，表明该区域当时水深相对较浅(图 1)。
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图 1 右江盆地构造位置(a)及其地质简图(b)(据Cai and Zhang, 2009; Hou et al., 2016修改) 图中各Sn(W)矿床的年龄数据来源于文献汇总(Wang et al., 2004；李水如等，2008；冯佳睿等，2011；Cheng et al., 2013；Mao et al., 2013; Xu et al., 2015) Fig. 1 Tectonic framework of the Youjiang basin (a) and its simplified geologic map (b) showing the distribution of Carlin-type gold deposits and igneous intrusions in the basin (modified after Cai and Zhang, 2009; Hou et al., 2016) Ages for the Sn (W) deposits are summarized from Wang et al., 2004; Li et al., 2008; Feng et al., 2011; Cheng et al., 2013; Mao et al., 2013; Xu et al., 2015 |
已有研究表明，右江盆地卡林型金矿的主要容矿岩石为晚古生代碳酸盐岩和中三叠统沉积碎屑岩，少部分为辉绿岩(Hu et al., 2002；Peters et al., 2007；Su et al., 2009a；Goldfarb et al., 2014)。从矿体形态上区分，碳酸盐岩容矿的金矿床往往发育层状矿体(如水银洞金矿)，而碎屑岩容矿金矿床的矿体则主要受高角度断层控制，其中以烂泥沟超大型金矿床最为著名(Zhang et al., 2003；Xia et al., 2012)。尽管容矿岩石和矿体产状不尽相同，但各卡林型金矿具有相似的矿物组合、矿床地球化学特征，暗示可能具有相似的成因机制(Hu et al., 2002；Zhang et al., 2003；Peters et al., 2007)。盆地内部构造活动强烈，并以北东和北西向断层最为发育，其中北西向右江大断裂可能控制了区内大多数金矿床的展布(图 1b；Peters et al., 2007)。具体而言，这些矿床主要发育于背斜的两翼或受控于次级断裂(Hu et al., 2002；Zhang et al., 2003；Su et al., 2009a； Xia et al., 2014)。
前已述及，除与峨眉山地幔柱相关的辉绿岩侵入体略显规模外，区内岩浆岩仅零星出露。在盆地北部出露一些碱性的超基性岩脉，该组岩脉距卡林型金矿床约30km(Su et al., 2009b)，锆石U-Pb定年结果显示其形成于85~88Ma(Liu et al., 2010c)。而在盆地的西侧，发育一系列沿北西和北东断裂分布的酸性脉岩。少量的定年结果显示，这些脉岩主要形成于90~100Ma(陈懋弘等, 2012, 2014)。此外，在盆地的南部和西部边缘，出露一些晚白垩世大型花岗岩侵入体，并产出一系列大型-超大型锡矿床(如个旧、大厂锡矿床，图 1b；Wang et al., 2004；Hu and Zhou, 2012；Cheng et al., 2013；Mao et al., 2013；Xu et al., 2015)。
3 样品与岩石学特征右江盆地的酸性脉岩主要出露于桂西北地区，其中大部分分布于卡林型金矿的外围(陈懋弘等，2012)，少部分与金矿床在空间上紧密相关。脉岩一般沿北东向和北西向断裂分布，倾角较陡。脉体宽度一般不超过20m，而走向上可延伸至20km。本文选取三处酸性脉岩开展研究，其中料屯和下巴哈两处脉岩分别横穿料屯和明山金矿矿区，而巴马脉岩与金矿床无直接空间联系(图 2)。
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图 2 巴马、料屯(a)和下巴哈(b)酸性脉岩分布地质图(据广西壮族自治区区域地质测量队，1971①修编) ①广西壮族自治区区域地质测量队. 1971.东兰幅(G-48-XXXVI)1:20万矿产图和田林幅(G-48-XXXV)1:20万地质图 Fig. 2 Geological distribution of the Bama, Liaotun (a), and Xiabaha (b) felsic dykes |
料屯脉岩沿龙田背斜核部发育的北东向断裂产出，倾角近乎直立。围岩地层有石炭系、二叠系灰岩及中三叠统百逢组砂岩-泥岩(属百逢组1~2段，图 2a)。该脉岩沿走向上延伸约10km，脉宽10m左右。采样点远离料屯金矿区，该处脉岩侵入至下二叠统灰岩地层中。岩石呈灰白色，斑状结构，其中斑晶主要为石英和白云母，粒径为0.2~2mm，含量约占10%；基质以石英、白云母和碱性长石为主，岩石学上可定名为石英斑岩(图 3a)。地球化学研究表明，料屯酸性脉岩富集硅(SiO2质量分数为75%~80%)和钾，属于过铝质S型花岗岩(李院强等，2014)。料屯金矿矿区内，矿体主要赋存于百逢组第2段砂岩-泥岩地层中，走向北西。石英斑岩脉沿北东向断层侵入至百逢组地层，近脉岩处砂泥岩发育显著硅化，同时切穿金矿体，暗示金成矿早于脉岩的侵位(陈懋弘等，2014)。
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图 3 料屯(a)和巴马(b)酸性脉岩显微照片(正交偏光) 矿物缩写：Kfs-钾长石；Mus-白云母；Qtz-石英 Fig. 3 Representative transmitted photomicrographs of the Liaotun (a) and Bama (b) felsic dykes (cross-polarized light) Abbreviations: Kfs-potassium feldspar; Mus-muscovite; Qtz-quartz |
下巴哈脉岩主要沿北西-北北西向断裂相间出露，倾角为60°~80°，脉宽约4m。其西北段主要侵入至石炭系碳酸盐岩地层中，向东南延伸约10km，且围岩逐渐过渡到二叠系灰岩及中三叠统百逢组1~2段砂岩-泥岩地层(图 2b)。采样点位于该脉岩的西北段。与料屯石英斑岩脉相比，二者具有相似的地球化学特征(黄永全和崔永勤，2001)；岩石学方面，斑晶以石英为主，白云母相对较少。该系列脉岩的东南段横穿明山金矿区，并侵入至下二叠统茅口组和中三叠统百逢组地层中(黄永全和崔永勤，2001；庞保成等，2014)。金矿体主要受近东西向断裂控制，赋存于百逢组第2段砂泥岩地层中；尽管未见脉岩与矿体直接的穿切关系，但二者显著斜交，可能不具有成因联系(庞保成等，2014)。
巴马酸性脉岩沿巴马背斜核部发育的北西向断裂产出，倾角近直立，出露宽度5~10m，走向上延伸近10km。与料屯和下巴哈石英斑岩脉不同的是，围岩地层除石炭系和二叠系碳酸盐岩外，还包括晚二叠世辉绿岩(张晓静和肖加飞，2014)；但未见脉岩侵入至中三叠世砂泥岩地层的地质现象(图 2a)。在采样点附近，该脉岩侵入至下二叠统灰岩地层中。岩石学方面，其与料屯石英斑岩脉相似，均为斑状结构，斑晶以石英和白云母为主，基质为石英、白云母和碱性长石(图 3b)；地球化学特征亦与料屯和下巴哈脉岩基本一致(陈懋弘等，2012)。
4 锆石U-Pb定年方法分别采集料屯、下巴哈和巴马石英脉岩约20kg(采样点见图 2)。为保证样品纯度，首先剔除了表面风化层，随后送至廊坊诚信地质服务公司挑选锆石。巴马脉岩挑选出的锆石较多(超过300粒)，以柱状自形晶为主，长度为100~200μm，长宽比一般为2:1。料屯和下巴哈脉岩的锆石含量较少，分别仅挑出50粒左右，自形程度较差，少量可见长柱状晶形，多为锆石碎片。颗粒一般较小，长度不超过100μm。为获得准确可靠的分析结果，基于上述锆石的不同形态特征，选取了不同的测试仪器和分析方法。
4.1 巴马酸性脉岩选取代表性的锆石约200粒制作环氧树脂靶，并拍摄透射光和反射光显微照片，以查明锆石的内部结构。上述工作在北京锆年领航科技有限公司完成。由于锆石颗粒较大，选择激光剥蚀-电感耦合等离子质谱仪(LA-ICP-MS)开展锆石U-Pb定年工作。该项测试在中国科学院地球化学研究所矿床地球化学国家重点实验室完成，使用仪器为193nm型准分子激光剥蚀系统(型号：GeoLasPro)和ELANDRC-e电感耦合等离子体质谱。测试期间，激光束能量密度为10J/cm2，束斑直径为32μm，频率为5Hz，剥蚀时间为40s。使用标准锆石91500矫正仪器质量歧视效应和元素分馏，而标准锆石GJ-1和Plešovice作为未知样，用以检验数据质量。单点分析的同位素比值及年龄误差为1σ。ICPMSDataCal10.2和Isoplot 3.76软件分别被用来处理原始数据和进行年龄计算(Liu et al., 2010a；Ludwig, 2012)。测得的锆石GJ-1和Plešovice的206Pb/238U加权平均年龄均与推荐值(GJ-1：~599.8Ma，Liu et al., 2010b；Plešovice：~337.1Ma，Sláma et al., 2008)在误差范围内一致。具体分析流程与Liu et al.(2010a, b)的描述相同。
4.2 料屯和下巴哈酸性脉岩将所有锆石样品并标样TEM2(416.8Ma；Black et al., 2004)和6266(559.0Ma；Stern and Amelin, 2003)用以制作环氧树脂靶。为揭示锆石的内部结构，完成透-反射光显微照相后，将锆石靶表面镀金并拍摄扫描电镜(SEM)、阴极发光(CL)和背散射(BSE)图像。所用仪器为蔡司公司生产的EVO MA15扫描电镜，并配有宽频CL和BSE探头。鉴于锆石颗粒较小，选择离子探针质谱仪(SIMS：Cameca IMS 1280)开展锆石U-Pb同位素测试工作。用强度为1nA一次O2-离子束轰击样品表面(轰击能量：23kV)，束斑为15μm×18μm。以上工作均在加拿大阿尔伯塔大学完成。用标准锆石TEM2校正样品的Pb/U比值，Th和U含量则通过标准锆石6266计算获得，并基于实测204Pb含量校正普通Pb。单点分析的同位素比值及年龄误差为1σ。原始数据处理采用SQUID2软件(Ludwig, 2009)，并通过ISOPLOT 3.76软件计算谐和年龄(Ludwig, 2012)。标准锆石6266的206Pb/238U加权平均年龄为560±1.5Ma(MSWD=2.4)，与其推荐值在误差范围内一致。详细分析流程请见Stern et al.(2009)。
5 锆石U-Pb年龄除原生结晶锆石外，3个酸性脉岩样品均富含数量不等的继承锆石。阴极发光图像显示大部分锆石都具有很好的岩浆环带(图 4a, d)。与结晶锆石相比，继承锆石晶形较差，多为锆石碎片，且边部形状不规则，可能暗示其遭受了不同程度的溶蚀；其他少量晶体较完整的锆石边部呈浑圆状或不规则状，暗示经历溶蚀或搬运、磨圆等沉积过程。原生结晶锆石的U-Pb年龄为95~100Ma，与陈懋弘等(2012, 2014)报道的白云母40Ar/39Ar年龄(95Ma左右)在误差范围内一致。继承锆石年龄显著较老，其206Pb/238U表面年龄主要集中于130~140Ma、242Ma左右、400~450Ma、700~1000Ma和1700~1800Ma等五个年龄段(图 5)。具体而言，各个脉岩中的继承锆石的特征和年龄略有不同。值得提出的是，由于前人已对上述脉岩的成岩时代进行了有效约束(陈懋弘等, 2012, 2014)，且本文的重点是通过继承锆石推测区内隐伏的岩浆活动并探讨其与金成矿的关系，因而对原生结晶锆石的U-Pb年龄不作深入讨论。
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图 4 料屯(a-c)和下巴哈(d-f)酸性脉岩中继承锆石U-Pb谐和年龄图 图a、d展示了代表性锆石的阴极发光图片，其中红色椭圆代表分析点位，并附相应点号(表 2).大部分锆石呈碎片状，且边部多由于溶蚀而呈不规则状；少量晶体较完整的锆石边部呈不规则状或浑圆状，暗示经历溶蚀或搬运、磨圆等沉积过程.图b、c和e、f中的红色椭圆代表ISOPLOT软件计算的谐和年龄范围(Ludwig, 2012)，分析点误差为1σ Fig. 4 Concordia diagrams of SIMS U-Pb isotopic analyses of inherited zircons for the Liaotun (a-c) and Xiabaha (d-f) felsic rocks Cathodoluminescence images of representative inherited zircons with spot numbers (red ellipse) are included in Fig. 4a, d, corresponding to the spot analyses given in Table 2. Note most of the zircons occur as fractions with irregular edges, and the relatively euhedral crystals have irregular edges or round shapes, indicative of corrosion or sedimentary processes including transportation and rounding. The red ellipses reflect the concordia ages calculated by ISOPLOT (Ludwig, 2012) in Fig. 4b, c, e, f. Data-point error ellipses are 1σ |
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图 5 酸性脉岩中继承锆石的206Pb/238U模式年龄分布图 Fig. 5 Frequency of 206Pb/238U model ages of the inherited zircons |
(1) 巴马酸性岩脉。该脉岩样品(BM)中的锆石以结晶期岩浆锆石为主，继承锆石相对较少。对35个锆石颗粒进行了LA-ICP-MS U-Pb定年，其中仅5颗属于继承锆石(表 1)。这些继承锆石的U=244×10-6~2076×10-6，Th=108×10-6~898×10-6，相应的Th/U=0.23~0.66。206Pb/238U年龄主要分布于400~450Ma和700~1000Ma两个时间段。
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表 1 巴马石英斑岩脉中继承锆石LA-ICP-MS U-Pb同位素分析数据 Table 1 LA-ICP-MS U-Pb isotopic data on the inherited zircons of the Bama quartz porphyry dyke |
(2) 料屯酸性脉岩。该脉岩样品(NJ)含有大量的继承锆石，而结晶期岩浆锆石相对较少。其中，很多继承锆石的晶形不完整(图 4a)。对样品NJ的27个锆石颗粒进行了SIMS U-Pb同位素分析，其中继承锆石为24颗(表 2)。这些锆石的Th和U含量变化较大(U=91.4×10-6~1410×10-6，Th=39.6×10-6~448×10-6)，但Th/U相对一致，除分析点NJ-B82@1和NJ-A10@1之外，所有分析点的Th/U均大于0.1(0.13~1.21)。U-Pb年龄涵盖上述五个分布区间(图 4a)。206Pb/238U年龄分布于242Ma左右和130~140Ma两个区间的锆石分别具有谐和的U-Pb同位素组成，与前者有关的11个分析点获得的谐和年龄为242.3±1.7Ma(2σ，MSWD=0.062；图 4b)，而与后者相关的3个分析点得到的谐和年龄为136.3±3.9Ma(2σ，MSWD=0.0006；图 4c)。
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表 2 料屯和下巴哈石英斑岩脉中继承锆石SIMS U-Pb同位素分析数据 Table 2 SIMS U-Pb isotopic data on the inherited zircons of the Liaotun and Xiabaha quartz porphyry dykes |
(3) 下巴哈酸性脉岩。下巴哈石英脉岩样品(XBH)的锆石也以继承锆石为主。由于锆石颗粒很小，仅选出11颗做SIMS U-Pb同位素分析，其中8颗为继承锆石(表 2)。这些继承锆石的U=169×10-6~4032×10-6，Th=36×10-6~640×10-6，除分析点XBH-A2@1和XBH-B5@1之外，Th/U比值均大于0.1(0.27~0.88)。U-Pb年龄分布范围较广，但集中于130~140Ma和242Ma左右两个时间段(图 4d)。前者含3个分析点，剔除一个明显发生Pb丢失的锆石，两个分析点获得的谐和年龄为128.2±2.3Ma(2σ，MSWD=2.9；图 4f)；而后者包括的3个分析点得到的谐和年龄为243.1±3.6Ma(2σ，MSWD=0.31；图 4e)。
6 讨论 6.1 继承锆石的成因锆石包括原生岩浆、继承、变质、热液等多种成因类型(Hoskin and Schaltegger, 2003；吴元保和郑永飞，2004；Schaltegger，2007；Yang et al., 2014)。而火成岩中的继承锆石大致具有两种来源：(1)捕获自围岩沉积岩地层；(2)来自于深部隐伏岩体。前者来自于碎屑锆石，常可以用来指示沉积的物源、沉积时代的上限以及重建古地理环境等(Gehrels et al., 2011；Thomas, 2011)。而后者则对指示隐伏岩浆事件的时代十分关键(Condie et al., 2009；Pereira et al., 2011)。
巴马、料屯和下巴哈酸性脉岩的形成时代为95~100Ma，围岩地层主要为晚古生代(C-T)碳酸盐岩和碎屑岩，均远远老于成岩时代(图 2)。其中最年轻的围岩为中三叠统百逢组1~2段(T2b1-2)。百逢组形成于三叠世安尼期，其1~2段的形成时代约为247~244Ma(Ovtcharova et al., 2006；Chen and Stiller, 2007)。因而，244Ma可以作为围岩地层中所含碎屑锆石的年龄下限。故我们获得的400~450Ma、700~1000Ma和1700~1800Ma等三个较老年龄段的锆石，很可能来自于围岩地层，而较年轻的130~140Ma的锆石应当来自于隐伏岩体。至于242Ma左右的继承锆石，其在误差范围内与百逢组1~2段近于同期，故上述两种来源均有可能。进一步的分析表明，该期锆石多呈碎片状(图 4)，具完整晶形者较少。此外，尽管料屯和下巴哈脉岩中该期锆石较多，而对未侵入至百逢组地层的巴马而言(图 2a)，并未发现242Ma左右的继承锆石(表 1)。因而我们认为，该期继承锆石更有可能捕获自围岩地层。
6.2 华南板块西南缘中三叠世岩浆事件及其动力学背景巴马、料屯和下巴哈脉岩中继承锆石的年龄主要分布于上述五个时间段，其中前三叠纪的三组年龄与华南板块主要的岩浆事件时限基本一致(Wang et al., 2012, 2013；Yang et al., 2012a)，暗示其可能与华南板块内部的各期岩浆事件相关。而130~140Ma的隐伏岩浆活动，则与华南板块140~125Ma时间段的岩石圈伸展较为吻合(毛景文等，2004；胡瑞忠等，2007b)，初步认为二者可能存在成因联系。
关于242Ma左右的继承锆石，由于其与最年轻的围岩地层(百逢组1~2段)近于同时代，结合岩层内部存在不少火山碎屑(Yang et al., 2012a)，表明岩浆与沉积事件相隔很短，也暗示沉积区域应紧邻242Ma左右(中三叠世)岩浆活动的中心。右江盆地南缘发育一些早-中三叠世的岩浆岩，尤以一系列火山岩的产出为代表(覃小峰等，2011；Yang et al., 2012b)。这些岩浆岩很可能为242Ma左右继承锆石的源岩。对于该期岩浆事件，存在两种可能动力学机制：(1)与太平洋板块西向平板俯冲有关(Li and Li, 2007；Carter and Clift, 2008；Li et al., 2012)；(2)受印支运动即印支板块与华南板块的相互作用控制(Zhou et al., 2006；Wang et al., 2013)。依照太平洋板块平板俯冲模型，右江盆地及其邻近区域应发育210Ma左右的岩浆活动，而240~250Ma的岩浆活动则应集中于华南板块的东南缘。显然，该模型无法解释上述中三叠世的岩浆事件。事实上，除南缘发育的火山活动之外，右江盆地周边也产出大量的早-中三叠世的火成岩。包括西侧的金沙江-哀牢山古特提斯带(Zhu et al., 2011；Zi et al., 2012；Lai et al., 2014；Liu et al., 2015)、越北地块(Roger et al., 2012)等。系列地质、地球化学证据表明，介于印支板块和华南板块之间的古特提斯洋闭合于中三叠世(245Ma左右)或略早，松玛缝合带(Roger et al., 2012；Faure et al., 2014；Lai et al., 2014；Wang et al., 2014)和/或介于右江盆地与越北地块之间的滇琼缝合带(Cai and Zhang, 2009)可能是古特提斯洋闭合后的残余(图 1)。因而，本研究涉及的242Ma左右的继承锆石所代表的岩浆事件可能与古特提斯洋的闭合紧密相关。
6.3 卡林型金矿与岩浆的可能关系尽管目前就右江盆地卡林型金矿的成矿时代争议较大，但较多的年龄数据表明这些金矿很可能形成于135~150Ma(Su et al., 2009b；王泽鹏，2013)或200~230Ma左右(陈懋弘等, 2007, 2009；Chen et al., 2015)。前者主要基于以下两点认识：(1) 金成矿与去碳酸盐化蚀变紧密相关；(2) 方解石为去碳酸盐化的产物，故认为方解石的Sm-Nd同位素年龄可以代表金成矿时代。200~230Ma左右的年龄主要来自于Re-Os同位素定年，所用样品为含金毒砂和含砷黄铁矿(陈懋弘等，2009；Chen et al., 2015)。最近，皮桥辉等(个人交流，2016)采用离子探针手段，对云南者桑金矿热液金红石进行了U-Pb定年，由于金红石与载金矿物——含砷黄铁矿具显著共生关系，推断者桑金矿形成于213.6±5.4Ma(MSWD=0.95)。该年龄与含砷黄铁矿、毒砂Re-Os定年结果在误差范围内一致。这表明右江盆地的卡林型金矿的早期成矿年龄可能为晚三叠世。
由上述讨论可以发现，右江盆地及周缘可能存在年龄在130~140Ma左右和约242Ma的隐伏花岗岩体。这两个时代的深部花岗岩浆活动与右江盆地两期卡林型金矿的成矿作用时代基本一致。这种时代上的一致性可能暗示，卡林型金矿的形成可能与其深部的岩浆活动具有成因联系。值得指出的是，这种推论是初步的，还需要更多成岩成矿精确年代学以及成矿流体地球化学的深入研究。
7 结论(1) LA-ICP-MS和SIMS锆石U-Pb定年表明，继承锆石主要集中于130~140Ma、242Ma左右、400~450Ma、700~1000Ma和1700~1800Ma等五个年龄段。对于较年轻的两个时间段，料屯和下巴哈石英斑岩脉捕获的继承锆石分别获得两组谐和年龄，分别为136.3±3.9Ma(2σ)和242.3±1.7Ma(2σ)、128.2±2.3Ma(2σ)和243.1±3.6Ma(2σ)。
(2) 前三叠世继承锆石应来源于围岩地层；130~140Ma锆石可能捕获自深部隐伏岩体，而242Ma左右的锆石颗粒与中三叠统百逢组近于同时代，进一步研究表明其可能来自于百逢组中的沉积碎屑锆石，该期锆石所代表的岩浆事件可能与古特提斯洋闭合有关。
(3) 右江盆地及周缘可能存在年龄在130~140Ma左右和约242Ma的隐伏花岗岩体。这两个时代的深部花岗岩浆活动与右江盆地两期卡林型金矿的成矿作用时代基本一致。这种时代上的一致性可能暗示，卡林型金矿的形成可能与其深部的岩浆活动具有成因联系。
致谢 在野外考察过程中得到中国科学院地球化学研究所肖加飞研究员、蓝江波博士、黄勇硕士、张晓静硕士及广西区域地质调查研究院潘艺文工程师的帮助；锆石U-Pb定年工作分别在中国科学院地球化学研究所戴智慧高级工程师和加拿大阿尔伯塔大学Richard Stern博士的协助下完成；胡瑞忠研究员对研究工作和论文的写作给予了指导和帮助；西北大学刘燊教授和另外一位匿名评阅人对文章初稿提出了许多建设性意见；在此一并表示感谢！| [] | Arehart GB, Chakurian AM, Tretbar DR, Christensen JN, McInnes BA , Donelick RA. 2003. Evaluation of radioisotope dating of Carlin-type deposits in the Great Basin, western North America, and implications for deposit genesis. Economic Geology , 98 (2) :235–248. |
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