2019, Vol. 35
中国西南特提斯处于世界特提斯构造带东端，是地质科学家颇为关注的研究区(图 1；莫宣学等, 1993；许志琴等，1996；张国伟等，1996；潘桂棠等，1997；殷鸿福和张克信，1997；钟大赉, 1998; 邓军等, 2011, 2012, 2014; Wang et al., 2017)。西南特提斯经历了增生-碰撞复合造山和壳幔结构的多期改造，导致成矿时间长、强度大、作用多样，复合成矿突出，是研究复合造山与复合成矿系统的理想选区，可揭示复合造山及其深部过程对复合成矿和金属富集的控制机制(图 2；李兴振等, 1999; 翟裕生等, 1999; 潘桂棠等, 2003; 李文昌等，2010; Zhang et al., 2014; Deng and Wang, 2016)。因此，深入研究该地区复合造山成矿作用，将为复合成矿系统理论的完善和成矿作用深部驱动机制的构建作出贡献，并为该区实现找矿突破提供有力的理论指导(邓军等，2011；Deng et al., 2017a, b, 2018a; Wang et al., 2018b)。
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图 1 中国西南特提斯及邻区构造框架图(据Wang et al., 2014a, 2016) Fig. 1 Geological map showing the tectonic framework of the SW Tethys of China and its adjacent areas (modified after Wang et al., 2014a, 2016) |
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图 2 中国西南特提斯造山带地质图(据Deng et al., 2014a, b) Fig. 2 Geological map of the SW Tethyan Orogen of China(after Deng et al., 2014a, b) |
为此，先后实施了两轮国家重点基础研究发展规划(“973”计划)项目“三江特提斯复合造山与成矿作用”(2009CB421000)和“中国西南特提斯典型复合成矿系统及其深部驱动机制”(2015CB452600)，其主要目的在于：通过对加里东期原特提斯洋消减与闭合、印支期古特提斯洋闭合与地块拼贴、燕山期中-新特提斯洋演化与陆内花岗岩省、喜山期碰撞造山重要地质事件的解析，查明复合造山过程与壳幔结构特征；通过对增生-碰撞造山岩浆热液型Cu-Mo-Sn-W、增生造山海底喷流型Cu-Pb-Zn-Ag、碰撞造山斑岩-矽卡岩型Au-Cu-Mo和碰撞造山盆地卤水-热液型Pb-Zn-Ag-Cu典型复合成矿系统的深入研究，探索增生造山VMS型、斑岩型和矽卡岩-云英岩型与碰撞造山斑岩型、矽卡岩型和MVT型成矿作用机理；通过解析矿带-矿田-矿床-矿体多尺度复合过程，揭示四类复合成矿系统形成的物质基础、流体活动和构造驱动等多因耦合关系，进而阐释复合成矿系统空间结构和深部驱动机制。
1 复合造山与构造体制转换机制复合造山是多期次造山以及其它类型壳幔过程在同一构造带先后发生或者多类型过程同时同位发生的地质事件。复合造山是大洋闭合-大陆拼贴过程的必然演化结果、地质历史时期普遍存在的地质过程、全球板块运动研究的薄弱区以及地球动力学研究的兴趣点(邓军等, 2016a, b；Deng et al., 2017a)。
研究区经历了原-古-中-新特提斯的增生造山和新生代碰撞造山过程。研究区古特提斯造山带是古特提斯构造领域的重要组成部分，且保留了大量有关古特提斯洋和分支海洋演化的岩石证据(Sengor, 1987; Schwartz et al., 1995; Metcalfe, 2002; Dupont-Nivet et al., 2010; Wang et al., 2014a, 2018a, c)。昌宁-孟连洋作为一个西南三江古特提斯造山带中典型的古特提斯洋，将东部思茅地块和西部保山地块分开(图 1; Metcalfe, 1988)。该缝合带北部与龙木措-双湖缝合带相衔接，南部与泰国清迈-茵他侬缝合带相连。前人研究集中在昌宁-孟连古特提斯洋的构造(Wu et al., 1995; Hennig et al., 2009; Peng et al., 2013; Deng et al., 2014a)，包括古特提斯洋的开启和闭合以及随后的沉积和碰撞过程(Sengor, 1987; Metcalfe, 1996, 1997; Ueno et al., 2003; 邓军等, 2012; Deng et al., 2014a)。然而，古特提斯的演变和不同阶段的时间约束仍然模糊不清，影响了对古特提斯演化和形成的全面了解。
昌宁-孟连缝合带经历了洋壳俯冲、陆陆碰撞和碰撞后伸展环境的演化过程，表现为多期岩浆活动特点(图 2; Ueno et al., 2003; 邓军等, 2011)。晚二叠世-早三叠世花岗质岩浆具有高钾钙碱性系列和I型花岗岩的特性，表现为从岛弧环境到碰撞后伸展环境的变化趋势。值得注意的是，早三叠世晚期-中三叠世花岗质岩浆年龄从250Ma到237Ma，花岗质岩浆具有S型和I型花岗岩特性，表现为从岛弧环境向碰撞后伸展环境转变过程(图 3；Deng et al., 2018b)。另外，早三叠世晚期-中三叠世的侵入岩发生一定程度变形或变质作用，亦表现为早三叠世和三叠系地层的角度不整合，形成于同碰撞环境(朱维光等, 2011; 毕丽莎，2014; Fan et al., 2015)。235~203Ma晚三叠世岩浆活动具有高钾钙碱性系列和A型花岗岩的特性，没有发生变形或变质，认为形成于碰撞后伸展环境，与金沙江-哀牢山缝合带的同时期构造环境相似(图 4；Zi et al., 2012a, b，2013; Deng et al., 2018b; Yang et al., 2019)。
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图 3 中国西南特提斯洋的演化过程(据Deng et al., 2018b修编) Fig. 3 Evolution of the SW Tethyan Ocean of China(modified after Deng et al., 2018b) |
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图 4 昌宁-孟连缝合带泥盆纪-三叠纪岩浆岩的地球化学图解 (a)Nb-Y图解；(b)Rb-(Yb+Ta)图解；(c)Rb-(Y+Nb)图解；(d)Rb-Hf-Ta图解(底图据Pearce et al., 1984; Pearce, 1996；Harris et al., 1986).数据来自赵靖等, 1994; 简平等，2003；Jian et al., 2009; Peng et al., 2008; 魏君奇等, 2008; Hennig et al., 2009; 朱维光等, 2011; 李钢柱等, 2012; 杨学俊等, 2012; Zi et al., 2012a, b; Deng et al., 2014a, 2018b; Wang et al., 2014b, 2015a, b Fig. 4 Geochemical discrimination diagrams of the Devonian-Triassic magmatic rocks from the Changning-Menglian Suture |
昌宁-孟连古特提斯洋的俯冲可能发生于中泥盆世，以蛇绿混杂岩的出现作为有力证据。俯冲相关的岩浆活动主要发生在晚石炭世-中二叠世。在晚石炭世发生的昌宁-孟连古特提斯的俯冲，持续到二叠纪-早三叠世，云县-景谷岛弧形成与此有关(图 5a)。思茅地块西缘的晚石炭世-中二叠世花岗闪长岩和镁铁超镁铁岩的侵入岩亦与昌宁-孟连古特提斯的俯冲有关(赵靖等, 1994; 魏君奇等, 2008; Hennig et al., 2009; Jian et al., 2009; 李钢柱等, 2012; Deng et al., 2014b; Wang et al., 2014a)。
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图 5 昌宁-孟连洋的构造演化过程 Fig. 5 Tectonic evolution of the Changning-Menglian Tethyan Ocean |
在早三叠世-中三叠世晚期，岩浆活动可能受古特提斯碰撞造山过程所控制，证据如下：(1)通过野外地质考察显示，上兰组和下伏的上二叠统羊八寨组间呈角度不整合，并且被中-晚三叠统火山沉积岩和早侏罗世的红色磨拉石所覆盖。这些火山沉积岩锆石U-Pb年龄为248.5±6.3Ma，表明在早三叠世晚期形成上兰组(Peng et al., 2008)。侏罗系与下三叠统呈角度不整合不仅在云县-景谷出现，而且在保山和思茅地区亦有出现，表明早三叠世属于同碰撞环境；(2)云县-景谷岛弧中芒怀组下段的安山岩被认为同碰撞环境的产物(朱维光等, 2011)；(3)一些岩浆岩被解释为在同碰撞环境中产生，如临沧岩基向北延伸的阿元山(约238Ma)(简平等，2003；Hennig et al., 2009; 杨明辉等, 2015)；(4)昌宁-孟连缝合带晚三叠世的变质和改造事件(毕丽莎，2014; Fan et al., 2015)。因此，早三叠世-中三叠世晚期岩浆活动合理解释为同碰撞环境，发生在早三叠世晚期-中三叠世之间，可能在250Ma左右(图 5b；Deng et al., 2018b)。
晚三叠世岩浆锆石年龄数据显示同碰撞到碰撞后环境的转换过渡(简平等，2003; Peng et al., 2008; Hennig et al., 2009; 朱维光等, 2011; Zi et al., 2012a, b; 杨学俊等, 2012; Wang et al., 2015b)。临沧花岗岩表现为高钾钙碱性特征，侵入年龄变化范围从234±1Ma到203±0.5Ma，岩浆活动最早发生在大约235Ma (Peng et al., 2013; Deng et al., 2018b)。云县-景谷地区芒怀组上段流纹岩在235Ma同碰撞环境下形成(朱维光等, 2011)。因此，从同碰撞到碰撞后的转换发生在晚三叠世，可能在235Ma左右。另外，Peng et al.(2013)和Hennig et al.(2009)报道，晚三叠世的流纹岩类似于云县-景谷地区非挤压背景所形成的A型花岗岩。云县-景谷地区的晚三叠世玄武岩具有与板块裂解有关的软流圈地幔的地球化学特征(Wang et al., 2010)。勐宋(大约222~228Ma)和布朗山花岗岩(约216~218Ma)，以及同时代辉绿岩主要产生于碰撞后环境(Wang et al., 2015a)。因此，我们提出晚三叠世岩浆岩形成于碰撞后构造环境(图 5c)。
区域构造演化与成矿动力学关系成为揭示成矿机理的瓶颈，探索成矿过程的构造控制及其驱动机制成为该领域的关键科学问题。针对该问题，对三江地区开展从矿物到巨型造山带尺度的构造变形、应力传递、流体流动和化学反应的系统研究，发现不同构造体制转换控制了区域成矿作用的类型与时空分布。通过系统地质证据标定和精细测年，识别出特提斯复合造山过程中215Ma大洋消减到地块聚合、130Ma洋壳俯冲到陆缘增生、65Ma增生到碰撞造山和35Ma岩石圈拆沉到陆内走滑四次构造转换事件，分别控制了斑岩型铜和VMS型铅锌铜银矿、层控矽卡岩型铜铅锌矿、云英岩型钨锡和矽卡岩型铜钼矿、斑岩型-矽卡岩型铜金多金属矿四次大规模成矿作用(Deng et al., 2014a, 2017a)。根据这些观察和全球对比研究，凝练出构造成矿动力学基本要点：构造动力体制转换是成矿的根本驱动，成矿参数临界转换是矿床形成的基本条件，构造-流体耦合是重要成矿机制，构造应力-应变场转变时空界面是主要成矿场所，从而揭示了构造体制转换成矿机理(Deng et al., 2014a)。
2 复合成矿系统理论复合成矿系统是复合造山构造转换时空域中不同时期多种成矿作用或者同一时期不同成矿作用复合形成的矿化网络、以及控制其形成与保存的全部地质要素构成的具有成矿功能的自然系统；其理论要点包括：多源复合的成矿物质来源、复合造山的成矿驱动机制、成矿流体运移的构造活化控制、构造转换复合的成矿机理、矿床破坏再生的变化过程、多类型矿种共存的保存条件(邓军等, 2016a, b; Deng et al., 2017a)。西南特提斯经历了原-古-中-新特提斯洋复合造山过程，发育多种类型和不同时代成矿作用复合成矿。为此，本文旨在确立西南特提斯复合造山过程中发育的不同成矿系统，揭示增生造山和碰撞造山成矿系统的相互关系，甄别出格咱斑岩型+矽卡岩型铜钼、扬子地块西缘斑岩型+造山型和保山-镇康矽卡岩型+热液脉型铅锌三条大型多金属复合造山带。复合成矿系统主要有增生造山海底喷流型Cu-Pb-Zn-Ag、增生-碰撞造山岩浆热液型Cu-Mo-Sn-W、碰撞造山斑岩-矽卡岩型Au-Cu-Mo和碰撞造山盆地卤水-热液型Pb-Zn-Ag-Cu(邓军等, 2016a, b)。西南特提斯典型复合成矿系统及其矿床特征列于表 1。
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表 1 西南特提斯典型复合成矿系统及其矿床特征 Table 1 Typical composite mineral systems and their characteristics of depsoits in the SW Tethys |
增生造山海底喷流型Cu-Pb-Zn-Ag复合成矿系统主要集中在昌宁-孟连缝合带老厂-铜厂街Cu-Pb-Zn-Ag和金沙江-哀牢山缝合带羊拉-鲁春Cu-Pb-Zn两个矿集区，尤其以产于洋岛火山(OIB)环境下的别子(Besshi)型的老厂Pb-Zn-Ag-Cu矿床最为典型(邓军等, 2016a, b)。在原特提斯洋和古特提斯主洋演化过程中，形成了与古特提斯洋岛环境火山岩有关的老厂VMS型Cu-Pb-Zn矿床(Li et al., 2015)。陈觅等(2010)报道了火山岩的SHRIMP锆石U-Pb年龄为323.6±2.8Ma，反映了VMS型Cu-Pb-Zn矿大致形成时间。老厂VMS型矿体主要受层位及构造控制，矿区主要出露有下石炭统依柳组火山-沉积岩。其中，硫化物在火山碎屑岩中尤为富集。火山碎屑岩为玄武岩、玄武安山岩、安山质和凝灰岩、角砾岩和集块岩等(冯庆来和刘本培，1993；陈百友，2002)。矿区内老厂背斜形态多样且为主要控矿构造。断层主要呈SN和NW走向，NE走向次之，其中SN和NW走向断层，主要控制老厂中心式火山喷发，矿体主要围绕火山喷发中心沉积洼地产出(叶庆同等，1992; 陈觅等，2010; 龙汉生等，2011)。矿体垂向可划分三层，在每层位发育大量块状硫化物矿体上下叠加(叶庆同等，1992)。矿体矿化分带明显，呈现“上黑(方铅矿-闪锌矿)下黄(黄铁矿-黄铜矿)”的分布特征(Li et al., 2015; 张鹏飞等，2017)。老厂VMS型矿体矿石呈现较均一硫同位素特征，δ34S值在-0.69‰~+1.32‰范围内，表明其成矿物质S主要来源于矿体下盘基性火山岩。流体包裹体属于NaCl-H2O体系，成矿温度为110~158℃，盐度为13.2%~18.7%NaCleqv，流体主要来自海底卤水(张鹏飞等，2017)。与老厂VMS型Cu-Pb-Zn矿床对比，昌宁-孟连缝合带还发育VMS型大坪掌矿床，赋存于弧后盆地双峰式火山岩中，成矿年龄为429±10Ma (Lehmann et al., 2013)，约束了该期的喷流成矿作用时限。老厂在印-亚大陆碰撞过程中，还发育斑岩-矽卡岩型Cu-Mo矿床，其矿石辉钼矿Re-Os等时线年龄43.8±0.8Ma(陈珲等，2010)。黑云母二长花岗斑岩侵位于下石炭统火山-沉积岩中。由深至浅，成矿类型依次为斑岩型钼矿化、矽卡岩型铁矿化和低温热液网脉型矿化(黄钰涵等，2017)。各类型矿石硫化物有较均一S同位素组成，δ34S值为-1.96‰~1.99‰(平均值+0.28‰)，与矿区斑岩硫同位素比较，老厂矿床符合还原型斑岩矿床特征(黄钰涵等，2017；赵晓勇等，2012)。
增生-碰撞造山岩浆热液型Cu-Mo-Sn-W复合成矿系统主要集中在腾冲-保山地块Sn-Cu-Pb-Zn和义敦岛弧Cu-Mo-W矿区。尤其以义敦岛弧成矿带发育的增生造山型印支期成矿(230~199Ma)和燕山期成矿(~80Ma)最为典型(Li et al., 2011; 李文昌等，2011; Yang et al., 2017)。义敦岛弧红山地区印支期三叠纪闪长玢岩的年龄集中于198~216Ma(徐兴旺等，2006；黄肖潇等，2012；刘学龙，2013；Peng et al., 2014；孟健寅，2014；王新松，2014)，岩体(87Sr/86Sr)i初始值为0.70485~0.70629，Pb同位素206Pb/204Pb比值为18.24~19.10，208Pb/204Pb比值为38.26~39.53，207Pb/204Pb比值为15.53~15.71；(143Nd/144Nd)i初始值为0.5122~0.5123，εNd(t)初始值为-0.89~-3.11，亏损地幔模式年龄tDM2为0.96~1.10Ga；εHf(t)值变化在-3.07~-9.55之间，模式年龄在tDM2为1.09~1.43Ga(黄肖潇，2013；孟健寅，2014)。李文昌等(2013)通过对成矿流体的研究发现，成矿流体中-高盐度NaCl-H2O体系热液主要源于印支晚期石英闪长玢岩的幔源岩浆活动；燕山期石英二长斑岩年龄集中于76~81Ma，与矽卡岩中辉钼矿和花岗斑岩中辉钼矿Re-Os同位素等时线年龄基本一致(77~81Ma)(徐兴旺等，2006；李文昌等，2011；王新松等，2011；黄肖潇等，2012；孟健寅等，2013；彭惠娟，2014；刘学龙等，2016)，表明燕山期是主要的斑岩-矽卡岩Cu-Mo多金属成矿期。花岗斑岩(87Sr/86Sr)i初始值为0.70475~0.70930，Pb同位素206Pb/204Pb比值为18.77~19.38，208Pb/204Pb比值为39.20~38.79，207Pb/204Pb比值为15.62~15.76；(143Nd/144Nd)i初始值为0.51204~0.51233，εNd(t)初始值为-4.04~-9.67，亏损地幔模式年龄tDM2为1.10~1.25Ga；而εHf(t)值变化在0.31~7.24，模式年龄在tDM2为0.67~1.02Ga(黄肖潇，2013；孟健寅，2014)。此外，流体包裹体、C-H-S和Re同位素表明燕山期含矿斑岩为同期的Cu多金属矿化提供了成矿热液和金属来源(李文昌等，2013；孟健寅，2014；王新松，2014)。
碰撞造山盆地卤水-热液型Pb-Zn-Ag-Cu复合成矿系统集中于兰坪-思茅盆地。王长明等(2017)将兰坪盆地发育的矿床划分为三种不同类型：中低温热液脉型Cu-Ag-Pb-Zn矿床、MVT Pb-Zn矿床和浅成低温热液型Sb-Hg-As矿床。其中，中低温热液脉型矿床Cu矿化主要发生于56~46Ma，浅成低温热液型矿床年龄集中分布于40~33Ma，中低温热液脉型矿床Pb-Zn矿化和MVT Pb-Zn矿床主要集中于33~21Ma。中低温热液脉型Cu-Ag-Pb-Zn矿床成矿温度变化范围为120.0~320.0℃，盐度变化范围为2.00%~24.00% NaCleqv，显示成矿流体以低温高盐度为特征的盆地卤水为主，其中金满-连城矿床受印度-欧亚大陆碰撞影响，成矿流体受到富CO2的变质水影响；MVT Pb-Zn矿床成矿流体变化范围为100.0~200.0℃，盐度通常变化于4.00%~16.00% NaCleqv，整体显示了低温、高盐度的盆地卤水特征；浅成低温热液型Sb-Hg-As矿床以笔架山Sb矿床为代表，成矿流体温度通常变化于120.0~160.0℃，盐度较低，整体上变化于0.00%~6.00% NaCleqv之间，成矿流体显示大气降水的特征(王长明等，2017)。因此，在兰坪盆地存在多期矿化事件复合成矿。
碰撞造山斑岩-矽卡岩型Au-Cu-Mo复合成矿系统与始新-渐新世富碱斑岩有关，集中于金沙江-哀牢山缝合带。北衙矿床有矽卡岩型和斑岩型两种类型矿体，存在叠加现象，代表多期岩浆活动的复合成矿(Deng et al., 2015)。其中，斑岩侵入体的年龄在34~38Ma，成岩高峰期为36Ma(和文言等，2012；Deng et al., 2015; Fu et al., 2015；Liu et al., 2015; 王建华，2017)；矽卡岩型Au-Cu-Fe矿床成矿年龄为~34Ma (和文言，2014；Fu et al., 2015, 2016)；热液型Pb-Zn-Ag(Au)矿化时代~32.8Ma(王建华, 2017)。斑岩型Au-Cu(Mo)矿床δ34S(‰)值为-1.6‰~+3.6‰；矽卡岩型Au-Cu-Fe矿床δ34S值为+0.2‰~+3.7‰；热液型Pb-Zn-Ag(Au)矿化δ34S值为-2.4‰~+1.5‰，三类矿床的δ34S值具有深源岩浆硫来源的特征，与北衙新生代富碱斑岩有直接关系(和文言，2014；王建华，2017)。斑岩型Au-Cu(Mo)矿床Pb同位素与富碱斑岩的Pb同位素值基本一致，表明三类矿床的矿化物质主要源于富碱斑岩(和文言，2014；王建华，2017)。流体包裹体研究的表明，矽卡岩型矿化成矿流体为高温的NaCl-H2O及NaCl-H2O-CO2体系热液；斑岩型矿化流体为中-高温的NaCl-H2O-CO2体系热液；热液脉型为中温的NaCl-H2O-CO2体系热液(王建华，2017)。三种类型矿床的包裹体特征表明北衙矿床的成矿流体主要来源于富碱斑岩演化的岩浆热液。
3 地壳深部结构和成矿机理前期研究工作采用“岩石探针”方法和地球化学示踪技术，结合重磁场线性构造提取技术，研究不同时序岩浆起源的可能源区和深部过程；探讨区域深大断裂与浅表构造之间的耦合关系；通过磁性体顶、底界面反演，分析壳内岩浆岩和变质岩空间分布特征；结合深地震反射剖面所揭示的高速体、低速体和拆离构造等分布，查明研究区内壳幔物质结构特征(Zhang et al., 2005)。三江地区兰坪-思茅盆地、保山-腾冲地块为大型莫霍面隆起区，表示地壳厚度较薄；然而江达-维西岩浆带、金沙江缝合带、义敦岛弧、临沧复合碰撞带和哀牢山造山带为局部幔拗带，表示地壳厚度明显增大(图 6；周道卿，2013；邓军等，2016a)。研究区各圈层均受到复合造山运动的强烈改造，包括保山地块、兰坪-思茅地块和东羌塘地块等莫霍面深度较浅，处于幔隆带内。主要造山带与莫霍面幔拗带具有较好的对应关系，表明造山过程中造山带内地壳快速增厚。隆拗结合带为板块间结合带或断裂发育地带(周道卿，2013；邓军等，2016a)。
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图 6 中国西南特提斯莫霍面特征(据周道卿，2013；邓军等，2016a) Fig. 6 Characteristics of the Moho surface in the SW Tethys of China (after Zhou, 2013; Deng et al., 2016a) |
尽管研究区构造演化和成矿作用的研究取得了一系列成果，然而在深部成矿驱动机制等尚存争议(Wang et al., 2014c; 邓军等, 2016a, b)。锆石Hf同位素地球化学填图不仅是探析岩石圈结构和演化等方面的重要手段，也是大地构造学和区域成矿学研究的热点和难点。国内外研究程度较低，不仅制约深部动力学理论完善提高，也影响矿产勘查实践的发展(Mole et al., 2012; Hou et al., 2015; Wang et al., 2016, 2017)。三江特提斯造山带因其独特的成矿地质环境和成矿作用过程，研究难度较大(Deng et al., 2014a; 杜斌等, 2016)。
系统收集西南特提斯成矿域Hf同位素数据，并对其进行统一处理，具体参数如下(Wang et al., 2016)：εHf(t)=10000({[(176Hf/177Hf)S-(176Lu/177Hf)S×(eλt-1)]/[(176Hf/177Hf)CHUR, 0-(176Lu/177Hf)CHUR×(eλt-1)]-1}; tDM=1/λ×ln{1+[(176Hf/177Hf)S-(176Hf/177Hf)DM]/[(176Lu/177Hf)S-(176Lu/177Hf)DM]}; tDMC=tDM-(tDM-t)([(fcc-fs)/(fcc-fDM)]; fLu/Hf =(176Lu/177Hf)S/(176Lu/177Hf)CHUR-1; fcc=[(176Lu/177Hf)平均地壳/(176Lu/177Hf)CHUR]-1; fs=fLu/Hf; fDM=[(176Lu/177Hf)DM/(176Lu/177Hf)CHUR]-1; (176Hf/177Hf)DM=0.28325; (176Lu/177Hf)DM=0.0384; (176Lu/177Hf)CHUR=0.0336; (176Hf/177Hf)CHUR=0.282785; (176Lu/177Hf)CC=0.015; λ=1.867(10-11 yr-1; t为锆石结晶年龄; 公式中字母的含义如下: S为样品，CHUR为球粒陨石均一储库，DM代表亏损地幔，CC代表大陆地壳。昌宁-孟连缝合带划分出了两个明显不同Hf同位素(εHf(t))和二阶段亏损地幔模式年龄(tDM2)的异常区。西部腾冲-保山地块和昌宁-孟连缝合带有低εHf(t)和高tDM2区域，高tDM2值很可能与古元古代区域的变质岩有关。东部地区的东羌塘、思茅块体和扬子地块出现了高εHf(t)和低tDM2区域，而中咱和义敦火山弧块体出现了一个低εHf(t)和高tDM2区域。低εHf(t)和高tDM2区域对应的是东部中-新元古代古老地壳基地组成。三个高εHf(t)和低tDM2表现东部较年轻的地体(图 7)。三维地壳结构图，从最西部的腾冲地块的遮放地区到最东部的扬子地块的宾川地区，显示了腾冲-保山地块上有大概38km厚的大陆地壳，其岩浆岩显示出低εHf(t)和高tDM2的特征，表明岩浆来源于古老的地壳或重熔的地壳(Zhang et al., 2005; Wang et al., 2016)。而扬子地块的大陆地壳厚度大约42km，显示出高εHf(t)和低tDM2值，表明了该区的岩浆岩来源于亏损的地幔(图 8; Zhang et al., 2005; Wang et al., 2016)。
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图 7 西南特提斯造山带Hf同位素εHf(t)等值线图(据杜斌等, 2016; Wang et al., 2016修编) Fig. 7 Hf isotopic contour maps showing the spatial variation of zircon εHf(t) value in the SW Tethyan Orogen of China (modified after Du et al., 2016; Wang et al., 2016) |
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图 8 西南特提斯造山带锆石tDM2 (a)、Hf同位素(b)和岩石圈结构(c)剖面图(据Zhang et al., 2005; Wang et al., 2016修编) Fig. 8 Profiles of zircon tDM2 values (a), zircon εHf(t) values (b), and lithospheric architecture (c) in the SW Tethyan Orogen (modified from Zhang et al., 2005; Wang et al., 2016) |
西南特提斯造山带晚侏罗世斑岩型Cu矿床和始新世-渐新世斑岩型Cu(-Mo)矿床沿甘孜-理塘缝合带和金沙江-哀牢山缝合带成群分布，εHf(t)值变化范围主要为0~2，tDM2年龄变化范围主要为1100~800Ma (Xiao et al., 2007; 郭晓东等, 2009, 2011; 邓军等，2010; Cao et al., 2016; Wang et al., 2016)。甘孜-理塘缝合带是古特提斯洋西向俯冲结束后，中咱地块与扬子地块的碰撞产物(Reid et al., 2007; Peng et al., 2008；冷成彪等, 2008; 2014; 曹殿华等，2009; Yang et al., 2011; He et al., 2013; Chen et al., 2014; Cao et al., 2016)。吴涛(2015)认为晚侏罗世斑岩发生了下地壳部分熔融，与俯冲背景下由软流圈上涌相关。如果这样，晚侏罗世斑岩和与之相关的铜矿床是发生在大约216Ma时俯冲板片撕裂引发的软流圈上涌之后，弧-陆碰撞时期形成或稍晚的环境，而不是在向西的俯冲过程中形成。此与环地中海带和环太平洋带的情况相似，斑岩型铜矿床不是形成于活动的向西的俯冲带，而是形成于地壳缩短/增厚时期或之后(Richards and Kerrich, 1993; Doglioni and Panza, 2015; Nimis and Omenetto, 2015)。三个高εHf(t)和低tDM2异常区沿着金沙江-哀牢山缝合带发育，对应始新世-渐新世钾质岩体和有关Cu-Mo、Cu-Au矿化，形成于后碰撞陆内环境。金沙江-哀牢山缝合带北部斑岩型Cu-Mo矿床的成矿年龄为40~36Ma，岩体锆石结晶年龄介于41Ma和37Ma之间(曾普胜等, 2006; Hou et al., 2007; Liang et al., 2007, 2008; 伍静等, 2011)。中部斑岩型Cu-Au矿化的时间为37~34Ma，与之有关的斑岩体的形成年龄为38~34Ma，近于同期形成(和文言等, 2011; Lu et al., 2012, 2013; 和文言, 2014; 蒋成竹, 2014; Deng et al., 2015)。南部斑岩锆石结晶年龄及与之有关的Cu-Au矿化的年龄集中于36~34Ma(王登红等, 2004; Liang et al., 2007)。此外，既有正值亦有负值的εHf(t)异常对应晚侏罗世花岗闪长岩岩体和与之相关的矽卡岩型Cu矿化。
早白垩世、晚白垩世和古近纪矽卡岩型和热液脉型Sn-W成矿系统发育于腾冲和义敦岛弧地体中，具有较老tDM2年龄值。这些岩浆岩与矽卡岩型和热液脉型Sn-W矿化有关，有相似的负εHf(t)值(-11.6~-3.9)、老的tDM2年龄(1800~1400Ma)、低的εNd(t)值(-14.7~-8.3)和相对较高的(87Sr/86Sr)比值(0.7104~0.7457)，指示了来源于中下陆壳的部分熔融(Xu et al., 2012; Ma et al., 2014; Chen et al., 2015)。白垩纪岩浆活动和与之相关的Sn矿化可能与中-新特提斯俯冲有关。然而，古近纪岩浆活动和与之相关的Sn矿化可能是碰撞后环境的产物(Ma et al., 2014; Wang et al., 2014b; Chen et al., 2015)。
晚三叠世-白垩纪矽卡岩型和热液脉型Pb-Zn-Cu-Ag矿化在空间上与元古代地壳块体有关。在腾冲-保山和义敦岛弧地体或金沙江缝合带显示出从正到负变化的锆石εHf(t)值，锆石εHf(t)值介于研究区斑岩型Cu-Mo-Au和花岗岩型Sn-W矿床之间(图 7)。晚侏罗世花岗闪长岩岩体和与之相关的矽卡岩型Cu矿化通常沿金沙江缝合带发育，锆石εHf(t)值(-3.7~+1.8)和中元古代tDM2年龄(1500~1100Ma)为特征，并捕掳了铁镁质微晶粒状包体，在晚碰撞或后碰撞构造背景壳幔混合形成(Wang et al., 2010; Zhu et al., 2011)。然而，晚白垩世侵入岩和与之有关的Pb-Zn-Ag矿床形成于后碰撞陆内伸展构造环境，以锆石εHf(t)值(-3.1~+0.2)和中-新元古代tDM2年龄(1300~1100Ma)为特征，来源于中-新特提斯俯冲和碰撞过程中-新元古代下地壳的部分熔融(Deng et al., 2014a, b; 李艳军等，2014)。以上研究不仅丰富了成矿系统理论，也对岩浆-热液型成矿区的找矿勘探提供重要指导。
4 找矿方法集成和重大突破在复合成矿系统理论指导下，揭示三江地区复合造山成矿具有矿床种类多样、矿床类型独特、构造转换控矿、叠加成矿显著、保存条件良好、成矿大器晚成、超大型矿床多以及矿床集约度高等特征。经过长期演化，三江地区形成了洋岛型、弧后盆地型、裂谷型和陆内裂谷型等四类VMS多金属矿床，俯冲型和碰撞型两类斑岩矿床，以及金顶和脉状铜铅锌矿等盆地容矿Cu-Pb-Zn矿床等多种矿床。前期建立的三江地区金顶铅锌矿、陆陆碰撞造山型金矿以及大陆碰撞型铜矿等特色大型矿床成因模式，较好地阐明了复合造山背景下的成矿作用。普朗斑岩铜矿作为格咱岛弧印支期中酸性斑岩成矿的代表，其研究成果指导格咱岛弧印支期斑岩-矽卡岩型铜多金属矿找矿实现了突破。此外，研究团队所提出的碰撞造山环境斑岩铜矿的成因模型，认为碰撞斑岩铜矿成矿斑岩为强烈挤压构造背景下形成的埃达克岩，成矿金属的深部富集是因岩浆高氧逸度所致。相比于国内外典型的增生造山型金矿，三江碰撞造山型金矿整体上具有矿石矿物组合复杂、成矿时代新、成矿流体幔源组分多盐度高以及壳幔相互作用明显的特征(Sun et al., 2009；李文昌等，2010；Deng et al., 2016a)。
在精细解剖三江特提斯成矿域的地质构造、矿产、物探、化探和遥感等信息基础上，对重磁推断深大断裂识别、隐伏岩浆岩体圈定、居里面、莫霍面隆起与坳陷区深部等异常信息进行了识别(图 9)。依据复合造山带构造体制转换成矿与叠加复合成矿等特征，并选取义敦岛弧、昌宁-孟连缝合带、保山地块、兰坪-思茅盆地和金沙江-哀牢山金铜成矿带等为重要远景区，开展了不同成因类型矿床勘查集成模式和隐伏矿体定位预测研究。依据不同规模、矿种、类型矿床的成矿模式以及勘查过程，对适用的勘查技术手段与类型(组合)的实施效果进行分析，选取适合三江高山深切割地貌、植被掩盖区的勘查技术集成技术。区域资源潜力评价以及找矿勘查技术创新成果在VMS和矽卡岩叠加型、俯冲型斑岩矿床、碰撞型斑岩矿床以及造山型金矿床等不同构造背景、多个构造单元、多种矿床类型勘查中起到了重要作用。在建立三江特提斯复合造山与成矿作用理论体系基础上，与地方生产单位密切合作，理论指导找矿，并取得重大突破(邓军等，2016a)。
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图 9 中国西南特提斯深部异常信息(据周道卿，2013；邓军等，2016a) (a)居里面；(b)莫霍面；(c)重磁推断隐伏岩体；(d)重磁推断断裂 Fig. 9 Deep abnormal information in the SW Tethys of China (after Zhou, 2013; Deng et al., 2016b) (a) Curie surface; (b) Moho surface; (c) concealed rock mass referred by gravity and magnetic field; (d) fault referred by gravity and magnetic field |
本文重塑了西南特提斯增生造山和碰撞造山构造演化历史，识别出特提斯复合造山过程中大洋消减到地块聚合、洋壳俯冲到陆缘增生、增生到碰撞造山和岩石圈拆沉到陆内走滑四次构造转换事件，它们分别控制了斑岩型铜和VMS型铅锌铜银矿、层控矽卡岩型铜铅锌矿、云英岩型钨锡和矽卡岩型铜钼矿、斑岩型-矽卡岩型铜金多金属矿四次大规模成矿作用。
确立西南特提斯复合造山过程中发育的不同成矿系统，揭示增生造山和碰撞造山成矿系统相互关系，甄别出格咱、扬子地块西缘和保山-镇康三条大型多金属复合造山带，解析其地壳深部结构和深部成矿驱动机理。
复合造山和复合成矿系统理论的提出得到国内外同行的高度评价，在找矿勘查中发挥了良好的社会经济效益作用，提高了中国学者在特提斯典型复合成矿系统及其深部驱动机制方面的研究地位，形成了具有一定国际影响力的构造成矿研究团队。
致谢 本文作者在多年的学习和工作过程中，一直得到翟裕生老师的指点与教诲。衷心感谢老师在矿床学领域研究的谆谆教诲和关心帮助，谨以此文恭贺老师九十华诞。论文的完成得益于与项目各课题负责人杨天南、王立全、许继峰、毕献武、孙晓明、李文昌、朱弟成的探讨；研究过程中，科技部联系专家马福臣研究员、赵振华研究员、许东禹研究员、顾连兴教授和丁悌平研究员，以及项目专家组成员翟裕生院士、滕吉文院士、莫宣学院士、侯增谦院士、潘桂棠研究员、张洪涛研究员、柴育成研究员始终给予了悉心指导和全力帮助，使项目按整体科学目标顺利实施。项目专家组成员以及“973”项目全体同仁的通力合作和共同努力，使得项目按预定目标整体推进，取得重要研究进展。谨此致谢。
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