2019, Vol. 35
2. 中国地质大学资源学院, 武汉 430074;
3. 香港大学地球科学系, 香港
2. Faculty of Earth Resources, China University of Geosciences, Wuhan 430074, China;
3. Department of Earth Sciences, University of Hong Kong, Hong Kong, China
铁氧化物-铜-金(Iron Oxide-Copper-Gold，IOCG)矿床是近20年来提出的重要矿床类型(Hitzman et al., 1992)，该概念曾把奥林匹克坝(世界第一的U、第五的Cu)、基鲁纳及白云鄂博(世界第一的REE)等世界上具有巨大经济价值，但成因争论较大的矿床联系在一起，引起国际上的巨大反响和关注。这类矿床储量巨大，含大量低Ti铁氧化物并伴生具有重大经济价值的Cu和Au，且不同程度地富集REE、U、P和Co等金属(Williams et al., 2005; Groves et al., 2010)。应该说，该类矿床是过去50年间继斑岩铜矿、块状硫化物矿、浅成低温热液金矿、卡林型金矿床之后的又一个重要矿床类型，具有显著的学术和勘查意义(毛景文等，2008)。国际上著名的IOCG矿床分布区域包括澳大利亚Gawler克拉通和Cloncurry地区、加拿大Great Bear地区、巴西Carajás地区以及南美洲中安第斯成矿带等。
经几十年的研究，国际上有关IOCG矿床的成因及勘查标志等方面已经取得不少进展(Barton and Johnson, 1996; Oliver et al., 2004; Xavier et al., 2008; Chen et al., 2010; Groves et al., 2010)。但相比于国外研究，国内的IOCG矿床研究起步较晚。在1992年IOCG概念提出后相当长的一段时间内，因缺乏详细、系统的个例研究，国内报道的典型IOCG矿床还很少。中国是否有典型的IOCG矿床？它们的成因如何？近年来，随着工作的深入，不少学者重新审视并详细厘定了国内不少区域的Fe-Cu矿床可能与IOCG矿床类似，并在矿床成因研究上取得不少重要进展(Zhao and Zhou, 2011; Chen and Zhou, 2012; Zhu and Sun, 2013; Li et al., 2014; Zhou et al., 2014; Hou et al., 2015; Hu et al., 2017; Zhao et al., 2017a, b; Liang et al., 2018)，也逐渐受到国内外同行的认可。本文在这些研究进展的基础上，概括中国IOCG矿床的分布及基本特征，并总结近些年来有关中国IOCG矿床成因方面的主要研究成果。除此之外，笔者就IOCG矿床的研究现状，对中国IOCG矿床的未来研究提出一些设想和展望。
1 IOCG矿床的定义和特点及成因进展简述铁氧化物-铜-金矿床概念的提出与20世纪70年代在澳大利亚南部Gawler克拉通中发现的奥林匹克坝(Olympic Dam)超大型铜-铁-金-铀矿床(含20亿吨矿石，包括35%铁、1.6%铜、0.06%铀氧化物、0.6g/t金及3.5g/t银)(Robert and Hudson, 1983)相关。最初提出的概念比较宽泛，把一系列看似没有成因联系的元古代富铁氧化物矿床如奥林匹克坝矿床、加拿大Wernecke和Great Bear矿床、美国Missouri东南矿床、瑞典的基鲁纳型铁矿(IOA)及中国的白云鄂博Fe-REE矿床等均归入其中。尽管如此，该矿床类型的提出促使学术界和工业界重新审视一些现有大型-超大型矿床的成因，并成功指导了一系列类似矿床的研究和勘查找矿。经过二十多年的研究，IOCG型矿床的定义逐渐完善(Williams et al., 2005; Groves et al., 2010)，不少学者把IOCG矿床进一步分成不同的亚类(Williams et al., 2005; Chen, 2013)。这些定义中，Williams et al. (2005)的提法认可度较高，其把IOCG型矿床进一步界定为具有大量低Ti磁铁矿-赤铁矿且伴生经济品位的铜(和/或金)矿化、构造控矿明显、与同期侵入岩无明显空间关系的热液矿床。之后，Groves et al. (2010)进一步深化并提出了狭义(sensu stricto)的IOCG概念，具体包括以下特点：1)发育大量低Ti磁铁矿-赤铁矿和/或铁硅酸盐矿物；2)伴生有经济价值的Cu和/或Au，且稍晚于Fe矿化；3)具明显的热液成因特点，且成矿受构造控制，常与角砾岩共生；4)常常不同程度富集REE、U、Ag、Co或P等其他金属；5)不含或极少含与硫化物同期的石英脉；6)与同期侵入岩无明显空间关系。基于该概念，一些含铁氧化物的矿床如磁铁矿-磷灰石(IOA)矿床、矽卡岩型Fe-Cu-Au矿床以及白云鄂博Fe-REE矿床等被剔除出去。从应用角度上而言，狭义的IOCG矿床概念不仅细化了判别标准，而且对之前有争议的矿床做了成因分类，使得IOCG矿床有了更明确的成因意义。
IOCG矿床的赋矿围岩类型多样，可包含近于同期或较老的火山碎屑沉积岩-火山岩、碳酸盐岩、基性-中酸性侵入岩、片岩-片麻岩等(Williams et al., 2005; Corriveau, 2007)，因此一定程度上也导致了不同IOCG矿床在矿化-蚀变特点上存在较大差别。但通常而言，IOCG矿床的成矿前主要是区域性/深部的钙-钠化蚀变，形成一些包括碱性长石如钠长石和/或钾长石或钙硅酸盐如角闪石等矿物(Skirrow et al., 2002; Corriveau, 2007)，甚至当围岩为碳酸盐时出现类似于矽卡岩的矿物组合(石榴石或透辉石等，如智利Candelaria矿床；Ray and Lefebure, 2000)；随后是铁氧化物的沉淀阶段，并伴随大量富Fe矿物的形成如铁-碳酸盐(菱铁矿和铁白云石)、富铁硅酸盐(绿泥石和阳起石)等(Williams et al., 2005; Corriveau, 2007)；之后的铜(金)成矿阶段主要有钾化而形成如钾长石、绢云母、黑云母等矿物以及碳酸盐化、电气石化、赤铁矿化等(Hitzman et al., 1992)。
现有研究结果显示，IOCG矿床基本上产出于克拉通或者大陆边缘的构造环境，并且大多数情况下与拉张背景密切相关，包括大陆裂谷环境(如Olympic Dam矿床)或者大陆边缘弧后盆地(如安第斯地区的IOCG矿床)等(Hitzman, 2000; Groves et al., 2010)。形成时代上，先前研究倾向于认为IOCG矿床具有前寒武纪成矿的时限性(如最初Hitzman et al., 1992及后来Groves et al., 2010的总结性文章)，也有学者把那些与岩浆-热液相关的IOCG矿床与斑岩铜矿相类比，认为他们代表了同类成矿系统在地球演化不同时期的产物(Richards and Mumin, 2013)。但无论如何，针对安第斯地区中生代(Chen et al., 2010, 2011, 2013a)和北美新生代(如美国Iron Spring矿床；Williams et al., 2005)及近年来新疆东天山古生代(Zhao et al., 2017a; Liang et al., 2018)IOCG矿床的很多个例研究，说明IOCG矿床在地质历史演化不同时期均可产生。但需要提及的是，在矿床的数量及规模上前寒武纪IOCG矿床确实更为显著(Groves et al., 2010)。
有关IOCG矿床金属及成矿流体的来源，虽然多年来积累了大量相关的研究资料，但该问题仍存在很大的争议，也因此在一定程度上影响到IOCG矿床定义的准确界定。例如Groves et al. (2010)的综述文章中突出了岩浆热液在IOCG矿床中的关键作用，他们认为狭义的IOCG矿床应为岩浆-热液型Fe-Cu-(Au)矿床，并且Fe、Cu、Au、REE等金属元素及金属络阴离子(如F、S、Cl等)等主要来源于岩浆(Groves et al., 2010)。相反，近年来不少研究证实，除了岩浆热液本身之外，矿床中的一些常见成矿元素如Fe、U、Co、S以及REE等可能有围岩或外来流体的巨大贡献(Chen and Zhou, 2015; Corriveau et al., 2016)。实际上，因缺乏直接的金属来源示踪方法，目前为止仍不清楚IOCG矿床中不同金属元素是否均来自同一种岩浆热液、抑或有多个源区。总体而言，有关流体来源主要有以下三种不同认识，包括: (1)成矿流体以岩浆-热液流体为主，外来流体(如盆地水)的加入对成矿并非关键(Pollard, 2000, 2006; Sillitoe, 2003)；(2)流体具混合来源(岩浆水、盆地卤水、层间水等的混合)，但岩浆水对早期铁矿化相对更重要(Kendrick et al., 2007, 2008; Baker et al., 2008; Chen et al., 2010, 2011)；(3)非岩浆流体(如海水、盆地卤水、大气水等)对成矿(特别是铜成矿)起主导作用(Barton and Johnson, 1996, 2000; Monteiro et al., 2008; Xavier et al., 2008)。
2 中国IOCG矿床的研究沿革Hitzman et al. (1992)提出IOCG矿床概念不到4年，国内已有学者把该篇论文翻译成中文(李上森, 1996)，但当时并没有引起国内学者的广泛关注。直到李泽琴等(2002)首次提出四川拉拉Fe-Cu矿床为IOCG型矿床以来，有学者开始对国内外IOCG矿床的研究进展进行了总结，包括张兴春(2003)、王绍伟(2004)、毛景文等(2008)及聂风军等(2008)。这些综述文章比较详细地介绍了全球IOCG矿床的特征和相关研究进展，并且对中国可能存在IOCG矿床的区域提出了一些展望，例如康滇、长江中下游、新疆东天山等地区。尽管这些文章把矽卡岩型Fe-Cu-Au矿、磁铁矿-磷灰石矿(玢岩铁矿或IOA)以及白云鄂博Fe-REE矿等目前看来不能归类为IOCG的矿床也归为其中，但一定程度上促进了国内学者对中国IOCG矿床的关注和研究(许德如等, 2008; 应立娟等, 2008; 路彦明等, 2010; 杜保峰等, 2012)。近些年来，国内有关IOCG矿床的详细、系统个例研究逐渐增多，取得不少重要进展，很多成果陆续在国内外的一些重要矿床杂志发表，引起国内外同行的广泛关注(Zhao and Zhou, 2011; Chen and Zhou, 2012; Zhao et al., 2013, 2017a, b; Zhu and Sun, 2013; Li et al., 2014, 2015b; Hou et al., 2015; Su et al., 2016; Liang et al., 2018)。上述研究表明，我国西南康滇地区、新疆东天山地区和东准噶尔北缘等地可能是重要的IOCG成矿带(图 1)，其具体分布特征如下：(1)西南康滇Fe-Cu成矿省，典型矿床包括四川拉拉、云南大红山及云南迤纳厂Fe-Cu矿床(Zhao and Zhou, 2011; Chen and Zhou, 2012; Zhao et al., 2015; Li et al., 2015b)；(2)新疆东天山阿齐山-雅满苏Fe-Cu成矿带，典型矿床包括黑尖山(Zhao et al., 2017a)、沙泉子(Jiang et al., 2018)、多头山Fe-Cu矿床(Zhang et al., 2018)等；(3)新疆东准噶尔北缘Fe-Cu成矿带，典型例子有老山口和乔夏哈拉Fe-Cu矿床(路彦明等, 2010; Li et al., 2015a; Liang et al., 2018; 梁培，2018)。其它矿区或矿带如新疆西天山阿吾拉勒成矿带(Hou et al., 2014a)、海南石碌Fe-Cu-Co矿区虽然也有部分矿床具有类似IOCG的特点(许德如等, 2008)，但目前仍存在不少争议且缺少从IOCG角度上进行的系统研究，它们是否属于IOCG矿床仍需更多的约束。
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图 1 中国大地构造略图及IOCG和似IOCG矿床的分布 Fig. 1 Simplified tectonic map of China and distributions of IOCG or IOCG-like deposits |
康滇Fe-Cu成矿省位于扬子克拉通西南缘(图 1)，南起元阳、北至会理，横跨四川南部、云南北部，多年来一直是中国重要的Fe、Cu产地(孙克祥等, 1991)。该区前寒武纪地层主要包括古元古代大红山群、东川群以及河口群和中-新元古代会理群、苴林群及昆阳群等；这些地层被一系列大大小小的元古代基性-酸性岩体所侵入(图 2a)，其中以新元古代花岗岩为主(830~760Ma; Zhou et al., 2002)。该成矿省有规模不一的Fe-Cu矿床20多个，包括大红山、拉拉、稀矿山、迆纳厂等大中型Fe-Cu矿床(图 2a)，主要赋存于古元古代沉积-火山岩地层中(即大红山群、河口群和东川群)。不完全统计，该成矿带已探明至少6亿吨Fe以及5百万吨Cu(孙克祥等, 1991; Zhao and Zhou, 2011)。除Fe-Cu矿床以外，区域上还分布有一套赋存于沉积岩中的层状Cu矿床(图 2a)，例如著名的东川和易门铜矿等(冉崇英, 1988; 华仁民, 1989; Ruan et al., 1991)，其矿化特点及矿物组合与Fe-Cu矿床明显不同，被认为沉积岩型层状Cu矿床(即SSC矿床；Zhao et al., 2012)。
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图 2 中国西南康滇(a, 据Chen and Zhou, 2012)、东天山阿齐山-雅满苏成矿带(b, 据Zhao et al., 2017a)和新疆东准噶尔北缘成矿带(c, 据Liang et al., 2018)地质略图及Cu-Fe矿床分布 Fig. 2 Simiplified geological maps and the distributions of major Fe-Cu deposits of the Kangdian Fe-Cu province (a, modified after Chen and Zhou, 2012), Aqishan-Yamansu metallogenic belt of East Tianshan (b, modified after Zhao et al., 2017a) and northern margin metallogenic belt of East Junggar (c, modified after Liang et al., 2018) |
该成矿省的Fe-Cu矿床在规模、围岩类型、金属品位和元素组合等方面虽有一定差别，但蚀变和矿化特征总体相似(表 1)。例如各矿床的矿体受构造控制明显(断裂、岩性界面等)，多呈透镜状、似层状(图 3a, b)；不少矿床中矿体与热液角砾岩空间关系密切，例如大红山矿床的部分矿体直接产于可能与同期辉长岩有关的角砾岩体中(图 3a、图 4a)(Zhao et al., 2017b)；大部分矿床与同期岩体没有明显的空间共生关系(Zhou and Zhou, 2011)等。矿石矿物为铁氧化物(磁铁矿/赤铁矿)和铜的硫化物(黄铜矿、斑铜矿)(图 4b)，但不同矿床中不同程度富集Au、Ag、Co以及REE等金属(孙克祥等, 1991; Zhao and Zhou, 2011)。例如拉拉矿床富集Mo、Co、LREE，其中Mo达到经济品位(Chen and Zhou, 2012)，而迆纳厂富集LREE和Co(Yang et al., 2005; Li et al., 2015b)等。研究显示，这些矿床均包括早期Fe和晚期Cu成矿阶段(图 5b)，并伴随早期区域性的钠化(钠长石、方柱石等)、Fe矿化期的Fe-Na-(Ca)蚀变(角闪石、钠长石、磷灰石等；图 5a)及铜矿化期的K化、碳酸盐化等(菱铁矿、云母、方解石等)(Zhao and Zhou, 2011; Chen and Zhou, 2012; Zhou et al., 2014)。
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表 1 中国IOCG矿床与世界典型IOCG矿床对比 Table 1 A brief comparison of China's and global IOCG deposits |
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图 3 不同IOCG成矿带中典型矿床的剖面图 (a)康滇地区大红山Fe-Cu矿床(据Zhao et al., 2017b修改)；(b)康滇地区拉拉Fe-Cu矿床(据Chen and Zhou, 2012修改)；(c)东准噶尔北缘老山口Fe-Cu矿床(据梁培, 2018修改) Fig. 3 Cross-sections of typical deposits in different IOCG metallogenic belts (a) Dahongshan Fe-Cu deposit in Kangdian (modified after Zhao et al., 2017b); (b) Lala Fe-Cu deposit in Kangdian (modified after Chen and Zhou, 2012); (c) Laoshankou Fe-Cu deposit in northern margin of East Junggar (modified after Liang, 2018) |
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图 4 不同IOCG成矿带中典型矿床的部分矿石野外特点 (a)康滇大红山矿床中块状Fe矿石与蚀变围岩(辉长岩)呈截然的接触关系(照片来自Zhao, 2010)；(b)康滇拉拉矿床中条带状Fe-Cu矿石被晚期富铜硫化物脉切穿；(c)东天山黑尖山矿床的Fe-Cu矿石中硫化物呈斑杂状分布于磁铁矿晶隙中(照片来自赵联党, 2018)；(d)东准噶尔北缘乔夏哈拉矿床Fe-Cu矿石中磁铁矿和硫化物与帘石矿物和石榴石紧密共生(照片来自梁培, 2018).矿物缩写：Mag-磁铁矿；Ccp-黄铜矿；Py-黄铁矿；Ep-绿帘石 Fig. 4 Field photos of Fe-Cu ores from different IOCG metallogenic belt (a) massive Fe ores in the Dahongshan deposit showing sharp contacts with hosting rocks (gabbro); (b) banded Fe-Cu ores in the Lala deposit crosscut by Cu-rich veins; (c) Fe-Cu ores in the Heijianshan deposit. Note that sulfides are present as interstitial phases in the magnetite matrix; (d) Fe-Cu ores in the Qiaoxiahala deposit, the magnetite and sulfides are associated with epidote and garnet. Mineral abbr.: Mag-magnetite; Ccp-chalcopyrite; Py-pyrite; Ep-epidote |
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图 5 不同IOCG成矿带中典型矿床的部分矿石镜下特点 (a)康滇大红山Fe矿石中磁铁矿与钠长石共生，交代早期铁白云石(照片来自Zhao, 2010)；(b)康滇拉拉Fe-Cu矿石中早期磁铁矿、磷灰石和钠长石被晚期硫化物、方解石和黑云母等交代、切穿，且磷灰石中还包裹细小的独居石颗粒(照片来自Chen and Zhou, 2012)；(c)东天山黑尖山Fe-Cu矿石中晚期黄铜矿切穿黄铁矿、磁铁矿及石英(照片来自赵联党, 2018)；(d)东准噶尔北缘乔夏哈拉Fe-Cu矿石中早期石榴石被磁铁矿、黄铁矿等交代(照片来自梁培, 2018).矿物缩写：Qtz-石英；Grt-石榴石；Ab-钠长石；Cal-方解石；Mnz-独居石；Ank-铁白云石；Ap-磷灰石；Bt-黑云母 Fig. 5 Photomicrographs of various ores in different metallogenic belts (a) Dahongshan Fe ore where early ankerite is replaced by magnetite and albite; (b) Lala Fe-Cu ore where early magnetite, apatite and albite are replaced by sulfides, calcite and biotite. The apatite contains abundant monazite grains; (c) Heijianshan Fe-Cu ore where early pyrite, magnetite and quartz are crosscut by chalcopyrite; (d) Qiaoxiahala Fe-Cu ore where early garnet is crosscut by pyrite and magnetite. Mineral abbr.: Qtz-quartz; Grt-garnet; Ab-albite; Cal-calcite; Mnz-monazite; Ank-ankerite; Ap-apatite; Bt-biotite |
新疆东天山地区是中亚造山带的重要组成部分，在古生代发育多个弧-盆单元，从北向南如大南湖-头苏泉岛弧带、阿齐山-雅满苏弧后盆地(或裂谷盆地)和中天山大陆弧等(图 2b)。该区域含有大量金属矿产，如Fe、Cu、Au、Ag、Pb、Zn等，是我国重要的铁铜多金属成矿带(Han and Zhao, 2003; Mao et al., 2005; 张维峰, 2016)。其中，阿齐山-雅满苏成矿带主要发育大量Fe和Fe-Cu矿床，它们赋存于石炭系海相火山岩地层中，因此曾被统称为海相火山岩型Fe-(Cu)矿床(图 2b)，典型例子包括雅满苏、多头山、黑尖山、双龙、沙泉子、双峰山、黑峰山等(Hou et al., 2014a; Zhang et al., 2014)。而新近研究所认为的IOCG矿床主要是指Fe-Cu矿床，如黑尖山、多头山、沙泉子等(Zhao et al., 2017a; Zhang et al., 2018; 赵联党, 2018)。该矿带上除主要发育这套赋矿火山岩外，还广泛分布有一系列中-酸性侵入岩体，但其与矿体之间无明显的空间共生关系。
相比于康滇IOCG矿床，该带的Fe-Cu矿床在规模上相对较小(多数 < 1万吨铜)，但矿体形态和主要矿石矿物组合与康滇矿床类似，例如其Fe-Cu矿体呈透镜状和似层状；矿石矿物主要是铁氧化物(磁铁矿/赤铁矿)和铜硫化物(黄铜矿、斑铜矿等)(图 4c)(赵联党，2018及其中参考文献)。矿化阶段均包括早期的Fe矿化(磁铁矿和/赤铁矿)和晚期的Cu矿化(黄铜矿和黄铁矿以及少量斑铜矿)阶段(图 5c)，但与康滇Fe-Cu矿床不同的是，不少矿床在Fe矿化之前都有明显的矽卡岩化(如多头山、沙泉子)而形成典型矽卡岩矿物如石榴石、透辉石、闪石等；Fe矿化具K化和Ca-Mg化而形成钾长石、角闪石、绿帘石等；Cu矿化期则有强烈的绿泥石化和/或绿帘石化等。除此之外，这些Fe-Cu矿床所含金属比较单一，除个别矿床局部富集Au(如黑尖山; Zhao et al., 2017a)，均无其它金属如REE、Co、P或Mo等的富集。
3.3 东准噶尔北缘Fe-Cu成矿带东准噶尔北缘位于东准噶尔地体北部的杜兰特岛弧带上，并以额尔齐斯大断裂为界北邻阿尔泰造山带南缘。该区主要发育一套上古生界火山-沉积系列，下古生界地层发育较少；岩浆岩广泛发育，以晚古生代碱性-钙碱性花岗岩和闪长岩为主、镁铁质-超镁铁质侵入岩次之(梁培, 2018)。该区矿产资源丰富，产出Fe、Cu、Au、Mo和Ni等多种金属，是新疆北部重要的矿集区。其中，前人所认为的类IOCG型Fe-Cu矿床产于上古生界火山-沉积地层中，典型例子包括老山口和乔夏哈拉Fe-Cu矿床(图 2c)(应立娟等, 2008, 2009; 吕书君等, 2012; Li et al., 2014; 尚海军等, 2017; Liang et al., 2018)，但其矿床规模均不大(表 1)。
这些矿床中，Fe-Cu矿体均赋存于泥盆纪北塔山组火山-火山角砾岩(以及少量沉积岩夹层)中，但部分矿床在时空上与闪长玢岩等岩体有一定共生关系；矿体呈似层状、透镜状产出(梁培, 2018)。Fe和Cu矿化在空间上并非完全重叠，因此矿体可分为Fe-(Cu)和Cu矿体，但两者呈渐变过渡关系且空间上呈现富铁矿体在上、富铜矿体在下的“上铁下铜”特点(图 3c)(李泰德和王梓嘉, 2009; 吕书君等, 2012; 梁培, 2018)。主要矿石矿物为磁铁矿和黄铜矿；成矿/蚀变期次包括成矿前矽卡岩化(或钙硅酸盐化)、Fe矿化阶段(磁铁矿)以及晚期的Cu矿化阶段(黄铜矿)。矽卡岩化形成大量石榴石、透辉石以及/或角闪石和绿帘石等(图 4d)，Fe矿化阶段蚀变矿物主要为角闪石、绿帘石和/或钠长石、钾长石等，而Cu矿化阶段的蚀变矿物则以绿泥石为主、绿帘石和石英等矿物次之(图 5d)(Li et al., 2014, 2015a; Liang et al., 2018)。总体而言，该成矿带除Fe、Cu矿化之外，金属组合比较单一，仅局部Au或LREE富集(应立娟等, 2006; 梁培, 2018)。这些矿床的矿化特点与阿齐山-雅满苏成矿带中的Fe-Cu矿床有很多相似点，例如一些矿床中出现显著的矽卡岩化(如老山口和乔夏哈拉)且其矽卡岩、矿体及岩体三者的时空关系密切(马玉鑫等, 2013; 梁培, 2018)。
4 中国典型IOCG矿床的成因研究进展虽然中国IOCG矿床的研究起步较晚，但近年来仍取得不少进展。总体而言，新疆东天山阿齐山-雅满苏和东准噶尔北缘成矿带相比于康滇成矿省在IOCG成因方面的研究相对较晚、研究程度稍低，并且在两矿带是否归属于IOCG矿床的问题上仍存在争议(如Mao et al., 2005; Li et al., 2014, 2015a; Jiang et al., 2018)。据于此，本文将以康滇IOCG成矿省为主，从矿床形成时代和构造背景、成矿流体特点等方面简要总结该区矿床的成因研究进展，而对东天山和准噶尔北缘的Fe-Cu矿床本文只做初步的总结。
4.1 康滇Fe-Cu成矿省 4.1.1 构造-岩浆-成矿时空格架新近不到10年的研究在康滇成矿省的赋矿地层、区域岩浆岩和矿床的形成时代上获得不少精确数据，基本完善了该区的构造-岩浆-成矿时空格架。首先在赋矿地层上，此前认为大红山群和河口群在时代上可能要老于东川群，而新近的锆石U-Pb精确定年基本确定三套地层的下部均形成于古元古代晚期(1750~1680Ma; Greentree and Li, 2008; Zhao et al., 2010; 周家云等, 2011; 王冬兵等, 2012; Chen et al., 2013b; 杨红等, 2012; 金廷福等, 2017)，代表了扬子陆块西缘古元古代晚期裂谷盆地沉积的一套火山-沉积建造(Wang et al., 2014)。一系列铁镁质岩体或岩脉等侵入至这套古元古代地层，它们的形成时代与地层近乎同时或稍晚(1750~1650Ma)，代表了一套大陆裂谷环境下的岩浆岩(Zhao et al., 2010; 关俊雷等, 2011; Chen et al., 2013b; Hou et al., 2015)。不整合覆盖于这套赋矿地层是昆阳群、会理群及苴林群，对其上部火山岩夹层的锆石U-Pb定年显示，它们形成于1100~960Ma左右(Zhang et al., 2007; 耿元生等, 2007; Chen et al., 2014a, 2018a)。但是最近对昆阳群和会理群下部火山岩地层获得了~1500Ma的年龄(耿元生等, 2012; 庞维华等, 2015)，限定其最老沉积年龄可达1.5Ga。该最老年龄与在东川群上部黑山组凝灰岩中获得的锆石U-Pb年龄(1503±17Ma)相当(孙志明等, 2009)，因此有学者认为东川群的上部与昆阳群的下部地层可能是连续的或者代表了同一个旋回沉积的产物(高林志等, 2018)。除此之外，新近研究也在康滇地区识别出一系列零星分布、形成于中元古代晚期的辉绿岩、辉长岩体及花岗岩体(~1050Ma; 如杨崇辉等, 2009; 朱志敏, 2011; 王子正等, 2012; Chen et al., 2018a)。这些岩浆岩的地球化学特征与该区同期火山岩(如苴林群和会理群天宝山组火山岩)一致，指示了它们可能形成于大陆裂谷环境(王子正等, 2012; Chen et al., 2014a, 2018a)。
近些年来，不少学者对这些矿床开展了系统的硫化物Re-Os、锆石U-Pb、褐帘石U-Pb等定年工作，获得不少可靠、精确的成矿年代数据(Zhao and Zhou, 2011; Chen and Zhou, 2012, 2014; Zhao et al., 2013; Zhu and Sun, 2013; 叶现韬等, 2013; Chen et al., 2018b; Zhu et al., 2018)。这些新数据显示，康滇Fe-Cu成矿省经历了多期成矿/热液事件，其中主成矿期包括~1.65Ga和~1.0Ga两期(图 6)。前一期的典型代表为大红山和迆纳厂矿床，与区域上一系列形成于板内环境的辉长岩/辉绿岩体同期，说明这些矿床形成于大陆裂谷环境；而后一期则以拉拉矿床为代表，时代上与区域~1.05Ga铁镁质-长英质岩体及相关火山岩相近，也说明该期矿化形成于大陆裂谷环境。有意思的是，该期矿化在大红山矿床有叠加，主要形成一些矿化脉体(宋昊, 2014; Zhao et al., 2017b)。除这两期主成矿年龄外，在迆纳厂和鹅头厂矿床的晚期脉中也获得~1.45Ga的硫化物Re-Os年龄(图 6)(Huang et al., 2013a)，可对应于区域上局部产出的同期基性岩体及昆阳群的火山岩夹层等，但该期矿化较弱，可能仅代表局部的热液活化或叠加事件。Zhu and Sun (2013)和Zhu et al. (2018)在拉拉矿床的Fe-Cu矿石中获得了一期~1.3Ga的硫化物Re-Os年龄，但区域上并未有相关岩浆事件与其对应，该年龄所代表的意义仍需进一步的研究和探讨。此外，早期Ar-Ar定年研究获得的大部分是新元古代的年龄(830~760Ma)(如邱华宁等, 1997, 2002; 叶霖等, 2004a, b)。目前已证实这些年龄代表了一期与该区新元古代岩浆岩相关的热液改造事件(Chen and Zhou, 2014; Zhou et al., 2014; Zhu et al., 2018)。
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图 6 中国不同IOCG成矿带中典型矿床的形成时代数据汇总 年龄数据来源: Zhao and Zhou, 2012; Chen and Zhou, 2011; 张志欣等, 2012; Huang et al., 2013a, b, 2014; Zhao et al., 2013, 2017b; Zhu and Sun, 2013; Zhu et al., 2018; Zhou et al., 2014; Li et al., 2014, 2015b; 赵联党, 2018; 梁培, 2018 Fig. 6 Summary of ages of Fe-Cu deposits in different metallogenic belts |
前人对康滇Fe-Cu矿床的流体包裹体开展大量研究，在成矿流体盐度、温度、成分等方面积累了丰富资料，提出了诸多认识(孙燕和李承德, 1990; 金明霞和沈苏, 1998)。近年来，不少学者又补充了流体包裹体的相关研究，进一步完善了该区矿床成矿流体的特征(侯林等, 2013; Li et al., 2015b)。这些研究显示不同矿床中Fe阶段成矿流体以高温(达500℃)、高盐度(达40% NaCleqv)的流体为主，显示岩浆来源的特点，而Cu矿化流体的盐度和温度明显降低。部分矿床(如迤纳厂)Cu阶段硫化物δ34S的值在0‰左右(图 7)，呈现典型岩浆硫的特征(Li et al., 2015b)，但是也有部分矿床硫化物δ34S的值呈现较大的变化，例如大红山矿床硫化物δ34S的值介于-3.4‰~12.4‰之间，拉拉矿床硫化物δ34S的值介于-5.3‰~10.5‰之间(图 7)，部分数值明显高于岩浆硫的范围(-5‰~+5‰)(Zhao and Zhou, 2011; Chen and Zhou, 2012)。这些数据显示，Cu矿化流体可能有岩浆流体和非岩浆流体或地层组分(如膏岩层; 华仁民, 1993)的加入有关。此外，不同矿床的C和O同位素也得到类似的结论。例如大部分碳酸盐矿物的δ13C和δ18O值与岩浆值比较接近(图 8)，说明有岩浆流体曾参与成矿；但也有部分δ13C和δ18O值与碳酸岩地层或地层水、盆地卤水及海水等比较接近(图 8)，说明岩浆流体可能与地层强烈相互作用或有外来非岩浆流体的加入导致成矿有关。
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图 7 中国西南康滇IOCG成矿省中典型矿床Cu成矿期的硫同位素组成(数据引自Zhao, 2010; Chen and Zhou, 2012) Fig. 7 Summary of S isotopic compositions of Cu-stage sulfides from typical deposits in the Kangdian IOCG metallogenic province (data from Zhao, 2010; Chen and Zhou, 2012) |
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图 8 康滇Fe-Cu矿床中不同阶段流体C-O同位素比值(数据引自Chen and Zhou, 2012; 王赕, 2013; Li and Zhou, 2015; Zhao et al., 2017b) Fig. 8 C and O isotopic compositions of carbonate minerals from typical deposits in the Kangdian region (data from Chen and Zhou, 2012; Wang, 2013; Li and Zhou, 2015; Zhao et al., 2017b) |
新近对热液矿物进行的原位B和Sr同位素研究也对康滇矿床的流体来源提供了新的制约。例如，Su et al.(2016)对大红山矿床中不同阶段电气石的B同位素做了细致的研究，其结果显示不同阶段电气石的B同位素组成具有系统的变化：早期钠化和Fe矿化阶段电气石具较轻的δ11B值(-14.7‰~-5.7‰)，与岩浆来源的硼非常接近；而Cu矿化阶段及最晚期热液脉阶段的硼同位素明显变重(分别为-4.4‰~-0.6‰和+2.9‰~+5.9‰)，说明有更多非岩浆流体参与成矿。同样，Chen et al. (2014b)和Zhao et al. (2015)分别对拉拉和迤纳厂矿床中不同阶段磷灰石进行原位Sr同位素分析。其结果均显示，早期铁矿化阶段磷灰石具低的87Sr/86Sr初始值(如迤纳厂：0.70377~0.71074)，与区域同时代岩浆岩比较接近，暗示岩浆流体参与成矿；而铜矿化阶段磷灰石具明显高的87Sr/86Sr初始值(如迤纳厂：0.71021~0.72114)，说明有外来非岩浆流体加入或发生过强烈水岩相互作用。总之，这些同位素分析结果与流体包裹体数据一致，均指示岩浆流体对早期Fe矿化成矿起主导作用，而晚期Cu矿化阶段则有更多的非岩浆流体参与成矿，并且流体混合或水岩反应可能促进了Cu成矿(侯林等, 2013; Zhao et al., 2015; Su et al., 2016)。
4.2 东天山阿齐山-雅满苏成矿带通过多年研究，获得不少有关该带赋矿地层和矿床形成时代的精确数据，基本完善了该区的岩浆-成矿时空格架。例如，大量的锆石U-Pb年龄新数据显示矿体围岩如雅满苏组和马头滩组火山岩分别形成于350~325Ma和325~305Ma(罗婷等, 2012; 张达玉等, 2012; Hou et al., 2014b; Zhang et al., 2016; 赵联党, 2018)；侵入至地层的中-酸性岩体主要以晚石炭世为主(如矿带较大的百灵山复式岩体)，最新年龄数据显示它们主要形成于330~300Ma且峰值为325±10Ma(徐璐璐等, 2014; Zhang et al., 2016; Jiang et al., 2017; 张维峰等, 2017; 赵联党, 2018)。多年来针对这些石炭系火山岩围岩及同期中-酸性侵入岩体开展了不少岩石成因和形成环境等方面的研究，但目前为止有关该矿带晚古生代的构造背景及演化仍然存在很大争议，包括有岛弧、弧后盆地以及后碰撞环境三种主要认识(赵联党，2018及其中参考文献)。除此之外，新近针对该区晚古生代岩浆岩的详细研究显示阿齐山-雅满苏矿带的晚古生代构造背景可能为弧前盆地，而Fe-Cu成矿主要发生于弧前盆地闭合期(Zhang et al., 2016; 赵联党, 2018)。成矿时代上，通过对部分Fe-Cu矿床(沙泉子、雅满苏、黑尖山等矿床)的精确定年研究基本限定这些矿床形成于295~320Ma(图 6)(Huang et al., 2013b, 2018; 赵联党, 2018)，大致与晚石炭世中-酸性侵入体同期。但是这些同期岩浆岩在构造环境上的争议一定程度上也间接导致了Fe-Cu矿床的成矿背景存在不少争议(袁峰等, 2010; 周涛发等, 2010; Pirajno, 2013; Hou et al., 2014a; Zhao et al., 2017a; Jiang et al., 2018)。
流体包裹体研究显示，阿奇山-雅满苏矿带中Fe-Cu矿床的成矿流体在Fe和Cu阶段存在明显差异性：早期Fe矿化流体具有高温(达590℃)、中高盐度(达56% NaCleqv)的特点，而Cu矿化流体则显示低温(低至160℃)、中-低盐度的特点(Zhao et al., 2017a; Jiang et al., 2018; 赵联党, 2018)。新近C-H-O-S同位素进一步显示，早期流体具有岩浆水为主的特点，而到后期Cu矿化流体则受到盆地卤水和/或大气降水的贡献较大(Zhang et al., 2018; Jiang et al., 2018)。
4.3 东准噶尔北缘成矿带该矿带赋矿地层以晚古生代火山-沉积岩为主，被一系列稍年轻的晚古生代中-酸性岩体侵入。新近锆石U-Pb定年结果显示，这些火山岩及岩体主要形成于两个期次：390~370Ma和360~325Ma(吕书君等, 2012; Wu et al., 2015; Liang et al., 2016; 梁培等, 2017; 梁培, 2018及其参考文献)。390~370Ma期岩浆岩显示有岛弧的地球化学特征，但其形成的构造背景存在有岛弧、弧后盆地甚至洋中脊环境等不同认识(Zhang et al., 2009; Long et al., 2012; Xu et al., 2013)。新近梁培(2018)对该矿带老山口和乔夏哈拉两个典型Fe-Cu矿床中的该期岩浆岩开展详细的岩石地球化学研究，证实它们形成于弧后盆地的构造背景，且整体处于盆地闭合的弧盆转化体系下。另一方面，360~325Ma的岩浆岩表现为A型花岗岩的特征，被认为可能形成于后碰撞至板内环境转化的过渡期(周刚等, 2009; 梁培等, 2017; 梁培, 2018)。对于Fe-Cu矿床的成矿时代，目前针对老山口和乔夏哈拉两个典型矿床的辉钼矿Re-Os、黄铜矿Sm-Nd定年工作显示Fe-Cu成矿时代为~380Ma(图 6)(张志欣等, 2012; Li et al., 2014, 2015a)。该年龄说明该矿带Fe-Cu成矿与区域390~370Ma岩浆作用同期，因此部分学者认为它们可能形成于弧后盆地的构造背景(Liang et al., 2018; 梁培, 2018)。
近年来有关该矿带成矿流体特点及来源的研究主要集中于老山口和乔夏哈拉Fe-Cu矿床，积累了大量数据(吕书君等, 2012; Li et al., 2014, 2015a; Liang et al., 2018; 梁培, 2018)。尽管不同学者对两个矿床的成矿期次划分不尽相同，但总体上主要包括成矿前的矽卡岩化阶段、Fe成矿和Cu成矿阶段(表 1)。研究显示矽卡岩化阶段的流体具高温(>550℃)、低-中盐度(< 20% NaCleqv)和类似于岩浆热液C-H-O同位素组成的特点(吕书君等, 2012; Li et al., 2014, 2015a; Liang et al., 2018)；Fe矿化流体具中-高温(< 530℃)、低-中盐度、高Mg/Fe的特点，但同位素数据显示除了岩浆流体外，海水的贡献明显增加；Cu矿化流体则具低-中温(低至160℃)、低-中盐度、富Ca或富Na的特点，稳定同位素及卤族元素组成数据显示该矿化流体具有大量盆地卤水或地层水的贡献，且晚期大气降水增多(Liang et al., 2018; 梁培, 2018)。
5 与全球IOCG矿床对比表 1总结了中国IOCG矿床与全球典型IOCG矿床在一些基本特征上的异同点，包括蚀变和元素组合、赋矿围岩类型、流体来源及演化、金属来源、成矿时代和构造背景等方面。与全球典型IOCG相比，西南康滇、新疆阿齐山-雅满苏和东准噶尔北缘等三个矿带的Fe-Cu矿床在矿化和蚀变特点上各有异同。但总体而言，康滇Fe-Cu矿床与世界上典型IOCG矿床(特别是前寒武纪矿床)更为相似，例如早期发育明显的区域性Na化、Fe矿化出现角闪石-钠长石化、晚期的Cu矿化出现K化等，矿体空间上常与角砾岩筒共生；除Fe和Cu之外，不少矿床含有经济价值的或明显富集Mo、LREE、U、P、Co、Au等(李泽琴等, 2002; Zhao and Zhou, 2011; Chen and Zhou, 2012; Hou et al., 2015; Li and Zhou, 2015)；矿化流体以岩浆流体为主、Cu矿化期外来流体贡献增加等。
另一方面，阿齐山-雅满苏和东准噶尔北缘矿带中不少Fe-Cu矿床矿化特点确实与典型的IOCG矿床(如前寒武纪矿床；Groves et al., 2010)存在一定差异。例如，两个矿带中Cu矿化相对较弱，金属元素组合单一(表 1)；大部分矿床早期都发育了显著的矽卡岩化，例如东准噶尔北缘的乔夏哈拉和老山口矿床，其矿体、矽卡岩及同期岩体在时空上紧密共生；部分矿床中矿体呈现“上铁下铜”的特点(如乔夏哈拉和老山口矿床)，与典型IOCG矿床正好相反。这些差异性一定程度上导致了这两矿带Fe-Cu矿床在是否能归属IOCG矿床的问题上目前仍存在不少争议，甚至部分学者根据这些矿床中普遍出现的矽卡岩类蚀变矿物更倾向于认为它们为矽卡岩型矿床(Mao et al., 2005; Li et al., 2015a)。但值得注意的是，这些矿床与典型矽卡岩矿床亦存在重要差别，例如多数矿床缺少空间上与矿体紧密共生的致矿岩体、缺少特征性的碳酸盐围岩、个别矿床并没有出现石榴石和辉石的干矽卡岩蚀变作用、另外很多矿床没有显示岩浆流体的明显贡献等(Hou et al., 2014a; Zhao et al., 2017a; Jiang et al., 2018)。因此，近年来不少学者通过对两个矿带构造演化的深入理解以及对部分矿床的详细对比，认为该带Fe-Cu矿床在蚀变和矿化特点、成矿流体特征以及构造背景上与南美中安第斯成矿带IOCG型矿床(如Mina Justa和Mantoverde矿床)相类似(Huang et al., 2013a; Li et al., 2014; Zhao et al., 2017a; Jiang et al., 2018; Liang et al., 2018；Zhang et al., 2018; 赵联党, 2018)。总之，随着今后研究的深入，有关两矿带的成因属性将得到进一步的约束和确认。
6 研究展望有关中国IOCG矿床的系统研究时间尚短，目前发现的IOCG或类IOCG成矿带还为数不多，但已有研究表明其分布广、时代跨度大、成矿差异明显。进一步加强我国类似矿床的研究，包括典例矿床的详细剖析和成矿带规律识别，不仅能极大促进我国IOCG成矿研究，也能丰富全球IOCG成矿理论的发展和相关矿产勘查的突破。笔者总结了以下几个今后中国IOCG研究可以进一步关注的方面：
(1) 东天山阿齐山-雅满苏和东准噶尔北缘成矿带Fe-Cu矿床的IOCG成因归属仍需进一步的确认。尽管近几年不少学者针对这两个矿带中几个典型Fe-Cu矿床的个例研究显示它们在蚀变组合、流体特点等与典型矽卡岩矿床存在明显差异(Zhao et al., 2017a; Liang et al., 2018)，但如前所述，部分矿床中侵入体、矽卡岩和矿体之间紧密的时空关系与典型的IOCG矿床存在差别。实际上，两个矿带中除这些类似IOCG的Fe-Cu矿床之外，区域上也分布有一些矽卡岩Fe矿床，这些Fe矿床与该区类IOCG型的Fe-Cu矿床在矿物和蚀变组合、成矿流体等方面究竟有何异同？显然，开展这两类矿床的相关对比研究可能为进一步确认这些Fe-Cu矿床的成因属性提供重要帮助。
(2) 进一步关注哀牢山-红河剪切带老基底中Fe-Cu矿床的成因研究。中国云南南部-越南西北部哀牢山-红河剪切带的老基底岩石中也发育一系列Fe-Cu矿床，典型例子包括中国境内的龙脖河和越南境内的新泉(Sin Quyen)矿床。不少研究认为这些矿床的矿化特征与IOCG矿床非常类似，并且有学者进一步推测它们可能原先是康滇IOCG成矿省的一部分，只不过后期被红河断裂沿东南方向错断且位移至目前位置(崔银亮等, 2004, 2005; Zhou et al., 2014)。然而，目前为止仍缺乏详细的相关对比研究。笔者最近对该带越南境内新泉矿床开展了定年研究，结果显示其主要矿化时代可能为新元古代(约840Ma)(Li et al., 2018; Li and Zhou, 2018)，可对应于康滇成矿省的后期热液改造年龄，但比成矿年龄略年轻。该年龄结果是否预示哀牢山-红河剪切带上的IOCG矿床与康滇成矿省没有联系？抑或有联系但代表了一期单独的矿化事件?显然，未来需加强哀牢山-红河剪切带上IOCG矿床的成因和成矿构造背景的研究，不仅对区域Fe-Cu勘探有重要作用，也将拓展中国IOCG的研究内涵。
(3) 深入研究矿床中铁和铜矿化的成因相关性。目前为止，有关中国IOCG矿床早期Fe矿化与后期Cu矿化的成因相关性仍存在不少问题没有解决。例如无论在康滇、东准噶尔北缘和东天山阿齐山-雅满苏地区，虽然成矿特点上均是以早期Fe矿化、晚期Cu矿化为主，但在空间上两者并没有完全重叠，稍有分离。究竟何种因素导致Fe和Cu矿化在空间上有部分分离、两者成因相关性如何？这些问题的解决不仅对了解IOCG矿床的成因提供重要的帮助，而且对完善世界IOCG矿床的成因有重要贡献。
(4) 关注中国IOCG矿床中多金属矿化的机制。中国不少IOCG矿床(尤其康滇成矿省)除Fe和Cu之外，还明显富集有REE、Mo、Co、Ni、U、Au、Ag等，与世界上典型IOCG矿床一致(Groves et al., 2010)。部分矿床中部分金属已达到工业开采或回收标准，例如康滇地区拉拉矿床中的Mo和Co等(王祝彬等, 2009)。实际上，这些元素的地球化学行为存在不少差别，例如Co、Ni通常与铁美质-超铁美质岩石相关，而REE、Mo、U等更倾向于在一些长英质或碱性岩中富集。究竟在何种条件、何种机制下这些元素均能富集于IOCG矿床中？遗憾的是，目前为止国内外针对此问题的研究仍然比较薄弱。笔者近几年来已经开始关注康滇地区IOCG矿床中的REE矿化，在REE活化特点及来源问题已经获得一些初步认识(Chen and Zhou, 2015; Li and Zhou, 2015, 2018)，但有关导致不同矿床中REE富集和矿化有差异的原因及REE与其它富集元素的关系等问题仍尚待进一步的约束。针对这些问题的研究，不仅能揭示IOCG矿床中不同金属的赋存状态及各元素富集之间的成因联系，还能为国家资源增储及金属选冶提供重要依据。
致谢 资料收集过程中，得到中国科学院广州地球化学研究所陈华勇研究员团队梁培和赵联党博士的慷慨帮助，在此表示衷心感谢。感谢硕士研究生刘磊在论文准备过程中完成了部分图件的绘制和数据收集。陈华勇研究员、李建威教授和胡瑞忠研究员审阅全文，并提出了许多建设性的意见和建议，在此致以诚挚的谢意！
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