2020, Vol. 36
2. 中国科学院矿产资源研究重点实验室, 中国科学院地质与地球物理研究所, 北京 100029;
3. 中国科学院地球科学研究院, 北京 100029;
4. 中国科学院大学地球与行星科学学院, 北京 100049;
5. 防灾科技学院, 三河 065210
2. Key Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China;
3. Innovation Academy for Earth Science, Chinese Academy of Sciences, Beijing 100029, China;
4. College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China;
5. Institute of Disaster Prevention, Sanhe 065210, China
纵观全球，浅成低温热液Au-Ag矿床、热液脉状Pb-Zn-Ag矿床与斑岩型Cu/Mo/Au矿床在空间上共同产出的现象比较普遍，例如保加利亚Southern Panagyurishte地区产出Cu-Au系统(Kouzmanov et al., 2009)，俄罗斯远东Koni-P'yagin半岛产出Cu-Mo-Zn-Pb-Co-Au-Ag-Bi系统(Sidorov et al., 2006)，秘鲁中部Morococha地区产出Cu-Mo-Pb-Zn-Ag成矿系统(Catchpole et al., 2011)，中国秦岭-大别地区产出Mo-Pb-Zn-Ag系统(李厚民等，2008；毛景文等，2009；Mao et al., 2011a；Zhao et al., 2018)，中国德兴产出Cu-Au-Pb-Zn系统(Mao et al., 2011b)，中国额尔古纳南段(秦克章等，1990；Qin et al., 1995)、东南沿海治岭头(Zeng et al., 2013；Wang et al., 2020)、大兴安岭南段车户沟(Zeng et al., 2011)、大兴安岭北段岔路口(金露英等, 2014, 2015)产出(Au-Ag)-Pb-Zn-(Cu)Mo系统等。
这些成矿系统中，研究最深入的是主要位于环太平洋成矿域的斑岩-浅成低温Cu-Au系统，在成矿系统模型(Sinclair，2007; Sillitoe，2010)、时空关系(Arribas et al., 1995; Marsh et al., 1997；Qin and Ishihara, 1998；Muntean and Einaudi, 2001；Masterman et al., 2005；Waters et al., 2011)、蚀变-矿化过程(Rye，1993；Hedenquist et al., 1998；秦克章，1998；Cooke et al., 2011；Franchini et al., 2011)、流体演化(Pudack et al., 2009; Deyell and Hedenquist, 2011)、金属运移-沉淀机制(Heinrich, 2005; Williams-Jones and Heinrich, 2005；Seo et al., 2012)、矿物及元素特征(Baumgartner et al., 2008；Chang et al., 2011；Deyell and Hedenquist, 2011；李光明等，2015)、构造背景(Qin et al., 2002；Cooke et al., 2005; Zhang et al., 2018；Wang et al., 2019)等多方面均取得了重要进展。
斑岩钼矿与热液脉状铅锌银矿是两种十分重要的矿床类型。过去所见更多的是二者独立产出，即不少斑岩钼矿周边并没有热液脉状铅锌银矿相伴，一些热液脉状铅锌银矿也没有斑岩钼矿相伴。究其原因，一则热液脉状铅锌银矿床向下蚀变仍然为线状或带状，没有转变为面状蚀变，或未进行深部勘查；二则部分斑岩钼矿剥蚀已到一定程度，即使上部和边部曾经发育有热液脉状铅锌银系统，也已剥蚀殆尽。近十年来，随着找矿勘查工作的深入进行，越来越多脉状铅锌银矿床在深部发现了斑岩钼矿化，例如满洲里甲乌拉铅锌银矿、云南老厂铅锌矿深部探获斑岩铜钼矿化(李峰等，2009)，大兴安岭北段岔路口矿床最初发现浅部脉状铅锌银矿化后，又在深部探获超大型斑岩钼矿(孟昭君等，2011)；此外斑岩钼矿床的周边也发现较多脉状铅锌银矿床，例如浙江治岭头先后发现了浅部金银矿化、深部钼矿化及外围脉状铅锌银矿化(Wang et al., 2020)。实际勘查成果表明，浅部热液脉状铅锌银矿化与深部的斑岩钼矿化之间，常常互为指示，因而研究成矿系统的主要特征、分析两类矿化共生与分离控制因素、查明两者之间的成因联系，对于理解斑岩成矿系统成矿过程、丰富成矿理论、指导区域矿产勘查具有重要意义。
本文通过收集目前该成矿系统的研究成果与勘查进展，总结出该成矿系统的基本特征、时空分布、岩浆特征及起源、蚀变-矿化特征、成矿物质来源、流体演化、金属分带和典型成矿系统勘查过程，在此基础上，提出该成矿系统的勘查标志及形成的若干要素，分析当前研究工作面临的问题并作出展望。
1 斑岩钼-脉状铅锌银成矿系统分布典型的斑岩钼-热液脉状铅锌银系统国外主要分布在北美西部，例如Colorado成矿带的Rico Mining地区(Larson，1987)，以及加拿大西南部不列颠哥伦比亚的Kitsault矿床(Steininger，1985)、Max矿床等(Lawley et al., 2010)。在中国，斑岩钼(钨)-热液脉状铅锌银成矿系统分布非常广泛(图 1)，主要集中在东部地区，包括秦岭-大别地区的南泥湖钨钼铅锌银矿田、付店钼铅锌银矿田和金寨钼铅锌银矿田等(李厚民等，2008；毛景文等，2009；Xu et al., 2011)，该区的典型矿床包括南泥湖-三道庄、东沟(Li et al., 2017；Jin et al., 2019)、沙坪沟(张红等，2011)、千鹅冲(李法岭，2011)等；华北北缘及西拉沐伦带也发育较多这类成矿系统，包括车户沟(Zeng et al., 2011)、劳家沟(曾庆栋等，2013)、大西沟(黄俊等，2012)、曹四夭(刘永慧等，2014；范海洋等，2018)、牛圈(沈利霞等，2012)等，该斑岩钼-热液脉状铅锌银系统还包括大兴安岭北段的岔路口(孟昭君等，2011)、满洲里地区的甲乌拉；此外，东南沿海的治岭头(王永彬，2014；赵超等，2014)、毛断(Li et al., 2012)、永定新村(韩胜康，2008)；西藏的亚圭拉(高一鸣等，2011)，湘南的黄沙坪(潘卓，2011；Li et al., 2016)和滇西的老厂(黄钰涵等，2017)也可能属于这一类成矿系统。
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图 1 中国斑岩钼矿-热液脉状铅锌银矿成矿系统分布 图中红色字体为钼铅锌银成矿系统 Fig. 1 The distributions of porphyry Mo-vein-sytle Pb-Zn-Ag mineralization systems in China Mo-Zn-Pb-Ag systems are labeled in red color |
根据前人和本文的研究成果，斑岩钼-热液脉状铅锌银系统，通常与高分异高演化的钙碱性花岗质岩浆相关(见下文)，成矿元素主要为钼(铜、钨)-铅-锌-银(金)，斑岩钼矿化与脉状铅锌银矿化两类矿化通常其中一类达大型，另一类为中小型，矿床可能含有萤石、磁铁矿等特征矿物，蚀变具有浅部粘土化-过渡带绢英岩化-深部钾硅酸盐化的分带，矿化具有上部或者外缘铅锌银矿化、下部及中心斑岩钼矿化的分带特征，两类矿化具有叠置关系或相距较近(见表 1)。其中，岔路口、沙坪沟、治岭头、东沟、千鹅冲、甲乌拉六个典型钼铅锌系统的大地构造位置、金属资源储量、平均品位、地层、构造、岩体特征、蚀变组合、成矿时代、成矿流体特征、钼铅锌银矿化空间关系等内容概述于表 2中。
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表 1 斑岩钼-热液脉状铅锌银系统基本特征 Table 1 Summarized features of porphyry Mo-vein-sytle Pb-Zn-Ag mineralization system |
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表 2 六个典型斑岩钼-热液脉状铅锌银成矿系统的地质特征 Table 2 Summarized geological characteristics of six selected porphyry Mo-vein-style Pb-Zn-Ag systems |
除上述基本地质特征外，该系统的确立需符合三个判定条件：(1)斑岩型钼矿化与热液脉状铅锌银矿化具有时空要素的耦合特征，两类矿化的时空框架一致(Sillitoe, 1973)。(2)两类矿化之间有着相互关联的地质因素，可表现为具有辉钼矿-闪锌矿-方铅矿矿物组合(如加拿大Max和中国岔路口)，也可以是构造断裂因素连接两种矿化类型等，例如脉状矿化与斑岩型矿化虽并不直接共生，但成矿热液沿着先存断裂就近沉淀形成脉状矿化(Redmond and Einaudi, 2010)。(3)成矿流体和成矿物质具有同源性和连续演化的特点，硫和铅同位素应指示岩浆成因(叶会寿等，2006b；王莹等，2019)，氢-氧同位素、流体的温度和盐度应出现连续演化的趋势(Lawley et al., 2010)。
3 各要素时空关系根据斑岩钼矿化与热液脉状铅锌银矿化的平面关系，钼铅锌银系统可分为近源和远源两类分布关系。斑岩钼矿化与热液脉状铅锌银矿化近源分布时，两者直接叠置或者平面距离一般小于2km，典型矿床包括我国千鹅冲(图 2a，李法岭，2011)、盖井(Xu et al., 2011)、毛断(Li et al., 2012)等，以及加拿大西南缘不列颠哥伦比亚的MAX矿床，与其周边的Lucky Boy和Copper Chief两个铅锌银矿床的距离小于2km (Lawley et al., 2010)；两类矿化远源分布时，其平面距离一般为不超过6km，例如东秦岭付店地区，三元沟、列山、西灶沟、老仗代沟、王坪西沟等热液脉状铅锌银矿床距离东沟斑岩钼矿的平面距离均在2~6km之间(图 2b，李厚民等，2008；Mao et al., 2011a)。钼铅锌银系统垂向上表现可为垂向叠置或者侧向分布，通常浅部脉状铅锌银矿化与深部斑岩钼矿化之间的垂向距离大多为500m，一般不超过800m，典型矿床包括治岭头(图 2c)、岔路口(图 2d)、甲乌拉、大西沟、劳家沟、沙坪沟等。
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图 2 典型斑岩钼-脉状铅锌银成矿系统平面和剖面简化示意图 (a)千鹅冲矿(近源实例，Li et al., 2017)；(b)东秦岭东沟矿集区(远源实例，Ye et al., 2008)；(c)浙江治岭头矿(垂向叠置实例，王永彬，2014)；(d)大兴安岭岔路口(垂向叠置实例，金露英等，2015) Fig. 2 Simplified geological maps and cross-sections for the typical porphyry Mo-vein-style Pb-Zn-Ag systems (a) Qian'erchong deposit (proximal example, modified after Li et al., 2017); (b) Donggou ore district, eastern Qinling (distal example, modified after Ye et al., 2008); (c) Zhilingtou deposit (vertically overlapped example, modified after Wang, 2014); (d) Chalukou deposit (vertically overlapped example, modified after Jin et al., 2015) |
成矿系统中两类矿化成矿时限关系，基于有限的数据可推测两者为同期形成，或者脉状铅锌银矿化相对略晚，但二者间隔通常最大不超过8Myr(表 3)。北美Rico区域的斑岩钼-热液脉状铅锌银系统，根据K-Ar年龄可知两类矿化近同期形成(Larson，1987)。加拿大MAX矿床辉钼矿的Re-Os年龄为80.3±0.2Ma，周边Lucky boy和Copper chief脉状铅锌银矿床中矿脉蚀变晕的白云母Ar-Ar年龄为72.2±0.5Ma，Lawley et al.(2010)认为这些周边的铅锌银矿化或者与80Ma的MAX斑岩钼矿化或者没有联系，或者是同一系统但K-Ar同位素体系在晚期的热液事件中被改变。我国秦岭-大别地区发育较为典型的斑岩钼-热液脉状铅锌银系统(毛景文等，2009；Cao et al., 2015；Zhao et al., 2018)，例如南泥湖成矿系统，前人研究获得南泥湖斑岩钼矿的辉钼矿Re-Os年龄为139~146Ma(叶会寿等，2006b)，周边冷水北沟、三道沟等脉状铅锌银矿床的绢云母Ar-Ar及闪锌矿Rb-Sr年龄，主要集中于137Ma。例如东沟钼矿化的辉钼矿Re-Os年龄为115~116Ma，周边同一成矿系统的三元沟、王坪西沟铅锌银矿床的绢云母Ar-Ar及闪锌矿Rb-Sr年龄为110~117Ma(Jin et al., 2019)。例如沙坪沟钼矿化的辉钼矿Re-Os年龄为111.1~113.6Ma，周边盖井铅锌钼矿化的辉钼矿Re-Os年龄为112.6~113.5Ma(Xu et al., 2011)。我国东南沿海治岭头矿床钼矿化的辉钼矿Re-Os年龄为113Ma，铅锌矿化的闪锌矿Ar-Ar年龄为113.9Ma(Wang et al., 2020)。受限于热液矿物Rb-Sr和Ar-Ar体系测得年龄能否准确反映铅锌银矿化形成时代的影响，例如后期热液时间导致同位素体系改变、同位素不均一、不封闭等因素干扰，成矿系统的精确热液时限尚需进一步深入。
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表 3 斑岩钼-热液脉状铅锌银成矿系统成矿时代 Table 3 Ages of porphyry Mo-vein-style Pb-Zn-Ag systems |
斑岩钼矿化多与酸性的高演化花岗质岩浆或者中酸性的钙碱性岩浆(Mutschler et al., 1981；Westra and Keith, 1981；Carten et al., 1993)相关。综合岔路口、千鹅冲等九个钼铅锌银系统的成矿岩体特征可知，该成矿系统的成矿母岩也多为高演化的钙碱性花岗质岩石，这类岩石的地球化学性质总结于表 4中。其主量元素通常呈现高硅(SiO2>71.0%)、高碱(K2O+Na2O为7 %~9%)、高钾(K2O/ Na2O为1.1~4.0)、高分异(分异指数>90)的特征，岩石性质属于偏铝或过铝质(ACNK为1~1.5)的钙碱性(里特曼指数σ为1~3)系列。成矿岩体一般富集K、Rb等大离子亲石元素，亏损Nb、Ta、Hf等高场强元素，且常相对亏损Sr、Ba、P、Ti等元素。成矿岩体的REE总量通常在60×10-6~250×10-6，稀土配分模式为轻稀土富集重稀土亏损的右倾铲状或海鸥型(图 3a)并具有Eu异常(δEu=0.4~0.7)。
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表 4 斑岩钼矿-热液脉状铅锌银矿系统成矿岩体地球化学特征 Table 4 Characteristics of the causative intrusions in the selected porphyry Mo-vein-style Pb-Zn-Ag mineralization systems |
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图 3 钼铅锌银成矿系统中成矿斑岩稀土元素配分图(a)和成矿元素Cu、Pb、Zn、Mo柱状图(b) 数据史长义等，2005；姚军明等，2005；包志伟等，2009；戴宝章等，2009；Lawley et al., 2010；杨梅珍等，2010；杨帆等，2012；Li et al., 2014b Fig. 3 Chondrite-normalized REE patterns (a) and group bar diagrams of concerntrations of Cu, Pb, Zn, Mo (b) in the causative porphyries in the selected porphyry Mo-vein-style Pb-Zn-Ag system Data from Shi et al., 2005; Yao et al., 2005; Bao et al., 2009; Dai et al., 2009; Lawley et al., 2010; Yang et al., 2010, 2012; Li et al., 2014b |
对于成矿系统中高硅岩体的源区特征研究，岩石的Pb-Sr-Nd-Hf同位素研究支持高氟、高品位斑岩钼矿(Climax型)的成矿岩浆大部分来源于古老下地壳部分熔融的假说，例如Climax、Henderson、Mount Emmons等(Stein and Hannah, 1985；Stein and Crock, 1990)。但中亚造山带中，以岔路口为代表的斑岩钼-热液脉状铅锌银矿床，成矿岩体具有较低的初始87Sr/86Sr比值(0.705413~0.707889)、εNd(t)值(-1.28~+0.92)、正εHf(t)值(+2.4~+10.1)及年轻的两阶段Nd和Hf模式年龄，地球化学和同位素数据表明其成矿岩浆起源于新生下地壳部分熔融，具有较高比例的幔源物质参与(Li et al., 2014b)。而部分与俯冲相关的钙碱性成矿岩浆，其源区则可能与斑岩铜矿的岩浆源区类似，通过壳-幔过渡带的MASH过程提供(Richards，2003)，例如沙坪沟、东沟、曹四夭、毛断等成矿系统的侵入体87Sr/86Sr比值为0.707268~0.7236，εNd(t)为-17.3~-11.17(图 4)，被认为起源于古老大陆地壳且加入了地幔物质(Wu et al., 2017；Ren et al., 2018a；Zhao et al., 2018)。
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图 4 钼铅锌银成矿系统中成矿岩体的Sr-Nd同位素组成 岩体数据引自Li et al., 2014b；Wu et al., 2017；He et al., 2016；Ren et al., 2018a；Wang et al., 2014；戴宝章等，2009；Yang et al., 2013.中国东北上地壳数据来自Wu et al., 2003；下地壳数据来自Othman et al., 1984；华北克拉通南北缘斑岩钼矿数据引自Li et al., 2014b及其参考文献；中国秦岭太华群数据引自Zhao et al., 2018 Fig. 4 The Sr-Nd isotopic compositions of the ore-forming intrusions in the selected porphyry Mo-vein-style Pb-Zn-Ag system Data of pluton from Li et al., 2014b; Wu et al., 2017; He et al., 2016; Ren et al., 2018a; Wang et al., 2014; Dai et al., 2009; Yang et al., 2013. Upper crust of Northeastern China from Wu et al., 2003; lower continental crust from Othman et al., 1984; porphyry Mo deposits in the North China Craton from Li et al., 2014b and the references therein; Taihua Group in Qinling Orogen from Zhao et al., 2018 |
结合前述主微量元素特征及分异指数可知，这类高硅岩体具有高分异特征，例如具有较高的Rb和Nb含量，东沟成矿岩体Rb和Nb含量为400×10-6~600×10-6和70×10-6~80×10-6 (Yang et al., 2015)；沙坪沟成矿岩体Rb为360×10-6~700×10-6，Nb为70×10-6~170 ×10-6 (Zhang et al., 2014)。结晶分异过程可促进不相容元素和挥发分元素富集(Candela，1997)，Mo作为不相容元素在岩浆结晶分异过程中相对容易富集在残余熔体中，会使得高分异花岗质熔体具有较高钼含量。同时，这种高分异岩浆中富集的高含量挥发分对金属的富集和运移通常起到重要作用(Kouzmanov and Pokrovski, 2012)，例如岔路口、沙坪沟等超大型矿床的形成即受益于高硅富碱富氟的岩浆成分和长期结晶分异的过程(Li et al., 2014b；Wang et al., 2014)。
钼铅锌银成矿系统的成矿岩体，与中国花岗岩中成矿元素的平均含量(史长义，2005)相比，Cu、Pb、Zn、Mo、W、Sn、Mn等虽有不同程度的富集，却并不太高(图 3b)，这可能是由于这些活动性强的金属元素从岩浆中大量进入流体，致使残余熔体结晶形成的岩石仅显示一定程度的富集(Audétat，2010)。随着LA-ICP-MS微量元素分析在熔融包裹体中应用，Climax型斑岩钼矿中熔体包裹体的元素成分逐渐被揭示，斑岩钼矿中成矿熔体并无异常高的初始Mo元素含量，成矿过程往往与后期热液演化-金属沉淀等过程相关(Audétat and Li, 2017)。例如Cave Peak斑岩钼矿中熔融包裹体的Mo含量5×10-6~12 ×10-6(Audétat，2010)、Pine Grove斑岩钼矿中熔融包裹体Mo含量为2×10-6~4×10-6(Audétat et al., 2011)、Urad-Henderson斑岩钼矿中熔融包裹体Mo含量为10×10-6~20×10-6(Mercer et al., 2015)，总体而言，大多数Climax型斑岩钼矿的成矿硅酸盐熔体为高氟(0.5%~4.0%)、高水(4%~9%)和低Mo含量(2×10-6~25×10-6)的高演化流纹质熔体(Audétat and Li, 2017)，表明要形成具有经济意义的钼矿，深部需要有大量岩浆提供金属元素。但钼铅锌银成矿系统的岩浆中钼、铅、锌、银等成矿元素的实际含量，仍需进一步开展微区精细分析。
5 蚀变-矿化特征前人对斑岩钼矿的蚀变矿化特征进行了一系列研究与总结(Sharp，1978；Wallace et al.，1978；Wallace，1995)。White et al.(1981)以美国Henderson矿床为例，结合其它的斑岩型钼矿，详细阐述了斑岩型钼矿床蚀变带的划分和特征，并认为斑岩型钼矿的主要蚀变带可与斑岩型铜矿相比较，即两者有相似的蚀变分带特征。赵俊兴等(2011)总结了世界上几个典型斑岩钼矿的蚀变特征，发现斑岩钼矿的蚀变分带基本上与其他斑岩型矿床相似：平面上呈现以岩体为中心的同心分带面状蚀变带，自内向外为钾硅酸盐化带(包括钾长石化和黑云母化)、绢英岩化带(石英-绢云母-黄铁矿化)、粘土化带(高岭土化和伊利石-水白云母化)、青磐岩化带(绿泥石-绿帘石-碳酸盐)，但垂向上则具有其他特殊的蚀变带，如Henderson的磁铁矿化和黄玉化，东沟的萤石化。另外斑岩钼矿还存在根据其他特殊蚀变矿物来定名的蚀变带，如脉硅化带、弥散性硅化带、磁铁矿和黄玉带、磁铁矿-黄铁矿带等。值得强调的是，含氟矿物是斑岩钼矿蚀变中的特征矿物，对高氟型斑岩钼矿更是如此。
斑岩钼矿体一般在成矿岩体上部呈披覆状产出，常见多层矿体，矿体形态也可为倒钟形(如Climax)、开放锥形或圆柱形(Mt Emmons，Ranta et al., 1984)、穹窿形和拳形(Carten et al., 1988)。当成矿岩体为多期侵入，且每期岩体形成不同的矿体时，最终的矿体形态为各期矿化叠加形成(Seedorff and Einaudi, 2004)。斑岩钼矿的矿化类型主要包括网脉状矿化、纹层状石英-辉钼矿脉、石英-辉钼矿-硫化物(及其他脉石矿物)脉、辉钼矿细脉、浸染状矿化、矿化角砾岩脉或角砾岩型矿化(如Boss Mountain，Soregaroli，1975；Questa，Ishihara，1967；Ross et al., 2002；鱼池岭钼矿，周珂等，2009)，多种矿化类型中以网脉状矿化和纹层状石英-辉钼矿脉最为常见。
前人对于热液脉状铅锌银矿的蚀变矿化研究并不深入，目前认为铅锌矿脉周边常发育的蚀变类型主要有硅化、绢云母化、伊利石-水白云母化、碳酸盐化、绿泥石化等(秦克章等，1990；孙丰月和王力，2008)。热液脉状铅锌银矿的规模和产状常受成矿断裂形态控制，与主断裂面有一定倾角的次级断裂、破碎带及角砾岩一般为主要容矿空间，产出含矿脉、细脉及块状矿石。由于含矿断裂控制了矿化，矿体可沿着断裂走向追踪，矿体最长可达1.5~2km(如甲乌拉)，垂向的矿化延伸则常有几百米甚至超1000m。此外，铅锌比值一般随深度变化，上部更富Pb，向下逐渐过渡至富集Zn，例如在俄罗斯北高加索地区的Sadon矿带，赋存在火山岩中的矿体，从矿化最顶部至1600m海拔标高，脉体中方铅矿占主导，Pb/Zn比值维持在3/1；在1400~1200m海拔标高，比值接近1/1；在900~700m海拔标高，Pb/Zn比值为1/(4~6)(Nekrasov，2007)。
较成型的斑岩钼矿-热液脉状铅锌银矿垂向共同产出的实例较少，根据岔路口、云南澜沧江老厂、湘南黄沙坪、千鹅冲剖面上的蚀变特征，可知成矿系统的蚀变特征通常为独立斑岩钼矿向热液脉状铅锌银矿的渐变，接触部位蚀变类型有叠加。自深向浅主要为钾硅酸盐化带、绢英岩化带、粘土化带、青磐岩化带，其中，粘土化带与绢英岩化带是两类矿床的叠加区。钼矿化常与钾化或者绢云母化带内侧密切相关(Seedorff et al., 2005；赵俊兴等，2011)，铅锌银矿化则常与浅部的绢云母-伊利石-水白云母化、碳酸盐化密切相关(秦克章等，1990；孙丰月和王力，2008；段士刚等，2011)。此外，根据Seedorff and Einaudi(2004)的研究，Henderson斑岩钼矿中发育其他钼矿中不常见的锰铝榴石带，该带覆盖粘土化带和绢英岩化带，其中该石榴石与一套方铅矿-闪锌矿-菱锰矿有关，是晚期热液事件的一部分。在这类两种矿化共存的系统中，常发育有典型钼铅锌银复合型脉体(金露英等，2014)，如岔路口的该类脉体是先存的石英-辉钼矿脉被之后的含铅锌脉体充填，形成含闪锌矿(-方铅矿)-辉钼矿的复合叠加脉体(图 5)，手标本容易辨认成同时沉淀的单一脉体。这类闪锌矿-辉钼矿脉脉宽5~30mm，规则，脉壁平直。脉体常具对称性，自脉壁向中心，依次为石英、辉钼矿、黄铁矿-闪锌矿-方铅矿±萤石。
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图 5 岔路口斑岩钼-脉状铅锌银成矿系统中典型的钼铅锌复合型脉体 (a)石英+闪锌矿(-方铅矿)+辉钼矿脉穿切早期石英脉；(b)石英+绢云母化岩体中的石英+闪锌矿(-方铅矿)+辉钼矿脉；(c)伊利石+水白云母化火山岩中石英+闪锌矿(-方铅矿)+辉钼矿+萤石脉，可见辉钼矿在脉体边部发育，闪锌矿和萤石处在在脉体中央；(d)斑岩钼矿中典型纹层状石英+辉钼矿+黄铁矿+闪锌矿-方铅矿脉，闪锌矿和方铅矿在脉体中央呈团块状产出 Fig. 5 Typical composite Mo-Pb-Zn vein in the Chalukou porphyry Mo-vein-style Pb-Zn-Ag mineralization systems (a) quartz+sphalerite(-galena)+molybdenite vein cut early quartz vein; (b) quartz+sphalerite(-galena)+molybdenite vein in the quartz+sericite altered intrusions; (c) quartz+sphalerite(-galena)+molybdenite+fluorite vein in the illite altered volcanic rocks, among which molybdenite distributed in the vein edge and sphalerite and fluorite occur in the center; (d) typical ribbon-textured quartz+molybdenite+pyrite+sphalerite-galena vein with sphalerite-galena clustered in the center |
斑岩型矿床研究中一个关键的问题是金属和硫的来源(Hedenquist and Lowenstern, 1994)。斑岩铜(±金，钼)矿的金属和硫来源主要为镁铁质岩浆已被大量研究所支持(Halter et al., 2002；Stavast et al., 2006；Stern et al., 2007)。而斑岩钼矿的金属和硫起源仍具有争议，一些研究者认为钼的来源由地壳主控(Candela and Piccoli, 2005；Seedorff et al., 2005；Sinclair，2007；Klemm et al., 2008；Song et al., 2019)。北美Colorado成矿带和秦岭钼成矿带中成矿岩体的Sr-Nd-Pb同位素证据都支持成矿岩浆源区为古老地壳物质(Johnson et al., 1990；Stein and Crock, 1990；Chen et al., 2000)。但过去也有部分研究成果支持钼主要来自幔源的镁铁质岩浆(Westra and Keith, 1981；Keith et al., 1986；Carten et al., 1993)。地幔起源的基性岩浆通过结晶分异作用可富集钼(Westra and Keith, 1981)，如Audétat(2010)对北美Cave Peak斑岩钼(铌)矿的熔融包裹体成分分析表明，在大陆裂谷背景下产生的镁铁质碱性岩浆，经过结晶分异作用，成矿岩浆中Mo的含量从镁铁质端元的4×10-6增加到12×10-6，形成了富钼的成矿岩浆。此外，基于北美西南部多个超大型斑岩钼(铜)矿(Rocky Mountains中部及东部)的铅同位素数据，Pettke et al.(2010)提出这些矿床中的钼起源于受俯冲流体交代的古老岩石圈地幔。因此，基于目前的研究可知钼来源具有复杂性和多解性(Ishihara and Qing, 2014)，需要更多的研究去进一步印证。
对于热液脉状铅锌银矿床，成矿物质的来源也存在支持岩浆来源或者地层来源的争论。部分学者支持岩浆来源，如Gökçe and Bozkaya(2006)对土耳其北部Inler Yaylasi铅锌矿的铅同位素研究得出其来源为造山带储库；Rice et al.(2007)对保加利亚Madjarovo的铅锌矿床运用硫同位素研究，认为成矿物质来源于火成岩和/或变质基底，但铅同位素数据更倾向于火成岩的源区；何鹏等(2018)对我国大兴安岭中南段扎木钦铅锌银矿的硫和铅同位素研究，认为成矿物质来自深源岩浆。还有部分学者重点强调地层或基底的作用，如Subías et al.(2010)对西班牙北东侧脉状铅锌(银)矿的同位素研究认为成矿物质主要来自于地层。而秦克章等(1990)则认为我国满洲里地区铅锌银主要来源于成矿母岩次火山岩，但围岩的作用也不可忽视。
斑岩钼-铅锌银成矿系统，硫、铅、锶、钕等多种同位素研究结果支持成矿物质主要起源于壳源岩浆(如南泥湖，叶会寿等，2006b；沙坪沟，张红等，2011；毛断，Li et al., 2012；曹四夭，Wang et al., 2017b)，通常具有不同程度的地幔物质和地层物质的加入。硫同位素结果显示，成矿系统中斑岩钼矿化的δ34S值主要位于-6‰~9.7‰，铅锌银矿化的δ34S值范围更宽主要在-3.1‰~12.1‰(图 6)，这些硫同位素范围虽大于岩浆硫范围(0‰±3‰，Ohmoto and Rye, 1979)，但与普遍报道的东北、秦岭-大别、扬子河、华南地区的钼矿化硫同位素特征一致(-6‰~10.2‰，Zhao et al., 2018及其引文；Wang et al., 2020及其引文)，且大部分位于I型花岗岩的硫同位素值范围(δ34S=1‰~9‰，Ishihara and Sasaki, 1989)，硫同位素被认为总体继承了岩浆硫的特征但可能有其他物质的混染，例如东沟钼-王坪西沟铅锌矿较高的硫同位素与熊耳组地层硫同位素一致，表明了地层物质贡献了硫等部分成矿物质(Zhao et al., 2018；Jin et al., 2019)。
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图 6 钼铅锌银成矿系统中硫化物的S同位素组成 数据来自Li et al., 2012；Liu et al., 2014；Zhang et al., 2014；金露英，2016；Ni et al., 2015；Wang et al., 2017a, 2017b, 2019；Zhao et al., 2018及其引文；Jin et al., 2019 Fig. 6 The S isotopic compositions of sulfides in the porphyry Mo-vein-style Pb-Zn-Ag system Data from Li et al., 2012; Liu et al., 2014; Zhang et al., 2014; Jin, 2016; Ni et al., 2015; Wang et al., 2017a, 2017b, 2019; Zhao et al., 2018 and references therein; Jin et al., 2019 |
成矿系统的硫化物铅同位素分析结果可知，斑岩型钼矿化的206Pb/204Pb、207Pb/204Pb和208Pb/204Pb比值分别为15.962~18.574、15.200~15.779和35.918~39.431，脉状铅锌银矿化的206Pb/204Pb、207Pb/204Pb和208Pb/204Pb比值分别为17.214~17.954、15.414~15.606和37.712~39.012。铅同位素图解(图 7)上显示大部分值位于造山带与下地壳演化线之间，且硫化物具有低-中等的放射性成因Pb同位素值和中等μ值(9.0~9.54)，低于上地壳μ值9.6，高于地幔μ值8~9(Zartman and Doe, 1981)，表明Pb具有下地壳和地幔混合的特征。前已述及，成矿系统中已知的Sr-Nd同位素结果也支持成矿岩浆形成于地壳熔融且加入了幔源物质。
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图 7 钼铅锌银成矿系统中硫化物Pb同位素组成(底图据Zartman and Doe, 1981) 数据来自Li et al., 2012, 2017；Liu et al., 2014；Ni et al., 2015；Wang et al., 2017a, b；Wu et al., 2017；Zhao et al., 2018及其引文；Jin et al., 2019 Fig. 7 The Pb isotopic compositions of sulfides in the porphyry Mo-vein-style Pb-Zn-Ag system (base map after Zartman and Doe, 1981) Data from Li et al., 2012, 2017; Liu et al., 2014; Ni et al., 2015; Wang et al., 2017a, b; Wu et al., 2017; Zhao et al., 2018 and the references therein; Jin et al., 2019 |
成矿流体的起源可用流体的氢-氧同位素进行追踪，斑岩钼矿化的流体主要为岩浆水，脉状铅锌银矿化的流体通常被认为是岩浆-热液成因(王祥东等，2014)，但部分矿床存在岩浆-热液成因与变质热液成因的争议。例如部分学者认为东秦岭-大别铁炉坪(陈衍景等，2003；Chen et al., 2004)、冷水北沟(祁进平等，2007)、沙沟(Han et al., 2014)、王坪西沟(姚军明等，2008)等脉状铅锌银矿床成矿热液起源于造山带变质热液，陈衍景(2006)对造山型银、铅锌矿床的特征和实例进行了系统总结；而另一部分学者则认为流体温度、成分及H-O同位素证据更为支持上述脉状矿为岩浆热液成因(Wang et al., 2013；Zhao et al., 2018)，且通过年代学、原位S、Pb及矿物微量元素研究，Jin et al.(2019)提出王坪西沟脉状铅锌矿与东沟斑岩钼矿属于同一钼铅锌成矿系统，为斑岩钼矿的远源矿化，表明王坪西沟矿床的岩浆-热液成因。虽然部分脉状铅锌银矿床的热液起源及其与斑岩钼矿的成因联系，尚需进一步通过多种方法进行多角度深入研究确定，但基于已知钼铅锌银成矿系统的H-O同位素结果(例如岔路口，东沟，沙坪沟，鱼池岭等)可知，与钼矿化相关的流体δDH2O值为-142‰~-52.79‰，δ18OH2O值为-4.2‰~8.5‰，同一系统中与铅锌银矿化相关的流体δDH2O值为-146.0‰~-54.5‰，δ18OH2O值为-13.9‰~13.9‰(图 8)，氢氧同位素特征显示成矿流体主要为岩浆水来源，铅锌银矿化时具有不同程度的大气水加入，铅锌银矿化流体继承了岩浆水性质并呈现连续演化的特征。
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图 8 钼铅锌银成矿系统中成矿流体的H-O同位素组成 数据来自Larson，1987；Yang et al., 2013, 2015; Liu et al., 2014；Zhang et al., 2014；金露英，2016；Ni et al., 2015；Wang et al., 2017a, b；王莹等，2019；Zhao et al., 2018及其引文 Fig. 8 The H-O isotopic compositions of ore-forming fluids in the selected porphyry Mo-vein-style Pb-Zn-Ag systems Data from Larson, 1987; Yang et al., 2013, 2015; Liu et al., 2014; Zhang et al., 2014; Jin, 2016; Ni et al., 2015; Wang et al., 2017a, b, 2019;Zhao et al., 2018 and the references therein |
成矿流体从岩浆中出溶的地质证据包括单相固结结构(Shannon et al., 1982；Lowenstern and Sinclair, 1996)、显微联通晶洞构造(Candela，1997；Harris et al., 2004；Audétat et al., 2008)等，例如典型的钼铅锌银成矿系统北美MAX矿床中，成矿岩体产出单相固结结构(Lawley et al., 2010)，我国东北岔路口钼铅锌银矿床的成矿岩体中产出单相固结结构、显微联通晶洞构造等多种记录流体出溶的结构(李真真，2014)。Lowenstern and Sinclair(1996)指出相比于无矿岩体，成矿岩体往往经历较大程度的岩浆、流体分异和出溶作用。同时该成矿岩体往往作为提供巨量金属和流体的深部岩浆房的重要通道(Sillitoe，1973)，一旦通道形成，大量成矿元素将从岩浆分配至流体中(Huber et al., 2012)，例如超大型沙坪沟矿床很可能形成于流体出溶后岩浆通道中的成矿元素和挥发分的高效对流(Wang et al., 2014)。学者们对岩浆热液流体的出溶过程进行细致研究并提出许多模型，包括气泡由重力作用从静态熔体中上升、流体通过多孔气泡连接的岩浆对流(Lowenstern，1994)、矿床下部导管内岩浆自身的对流(Shinohara et al., 1995)等。除少数报道斑岩系统中初始流体可能是高盐度流体(>50.0%NaCleqv，Li et al., 2011)，通常认为斑岩系统初始流体为单相中低盐度(Klemm et al., 2007, 2008；Pudack et al., 2009；Allan et al., 2011)，而后期普遍发育的含石盐子晶包裹体和富气相包裹体则是由该初始流体发生沸腾或不混溶形成的(Rusk et al., 2008)。
热液脉体可记录成矿流体演化过程中温度、盐度、成分等信息的变化。斑岩型矿床中，热液脉体通常可分为早期含磁铁矿的M脉(Arancibia and Clark, 1996；Ulrich and Heinrich, 2002)、弯曲的A脉(Gustafson and Hunt, 1975)、EB(黑云母)脉(Gustafson and Quiroga, 1995)，主成矿期的B脉和D脉(Gustafson and Hunt, 1975)，以及成矿晚期的G脉(李光明等，2007)、石英-绿泥石脉(Sillitoe，2010)等。
目前钼铅锌银成矿系统各阶段的流体温度、盐度特征具有较多报道(沙坪沟，Ni et al., 2015；东沟，Yang et al., 2015；千鹅冲，Yang et al., 2013；鱼池岭，Zhang et al., 2014；岔路口，Liu et al., 2014；Li et al., 2019；治岭头，Wang et al., 2017a；曹四夭，Wang et al., 2017b)，但整个系统的演化过程、初始流体特征及成矿元素含量等方面精细研究仍较为薄弱。对早期A脉的研究表明，单一斑岩钼矿床的初始流体通常为单相中低密度流体，例如Questa斑岩钼矿的最早期流体为单相含CO2的低盐度流体(~7% NaCleqv，Klemm et al., 2008)，单相流体可能具有~100×10-6的金属钼含量(Audétat and Li, 2017)。钼铅锌银系统的A脉也呈现高温单相中低密度流体特征(例如岔路口，金露英，2016；Li et al., 2019)。伴随着减压沸腾作用、大气水加入、流体冷却以及水岩反应的进行，成矿流体常形成大规模的钾硅酸盐蚀变以及绢英岩化蚀变，并发生大规模的钼矿化，沉淀出含辉钼矿的B脉，其温度区间通常在300~450℃(杨永飞等，2009；Lawley et al., 2010；Li et al., 2019)。该流体持续降温，混入较多大气水后，则会形成粘土化蚀变以及外围的青磐岩化蚀变，并发生浅部的脉状铅锌银矿化，形成含闪锌矿-方铅矿的D脉或者宽几米至几十米的大脉，该阶段的流体呈现中低温中低盐度的特征，温度区间在175~320℃，盐度区间在0.6%~5.5%NaCleqv (Larson，1987；Lawley et al., 2010；Li et al., 2019；王莹等，2019)。
8 金属沉淀和分带携带大量成矿金属元素的流体自出溶后的演化过程则是理解沉淀机制的关键。岩浆热液流体在气液相的分离过程中，大部分的Zn、Pb、Mo、Ag等金属元素倾向于进入高盐度流体中(Ulrich et al., 2002；Heinrich，2005；Pokrovski et al., 2005；Williams-Jones and Heinrich, 2005；Simon et al., 2007；Audétat et al., 2008；Nagaseki and Hayashi, 2008；Pudack et al., 2009)，且成矿流体中这些成矿元素含量相近，甚至部分矿床的Zn、Pb、Ag含量比Mo含量更高，即矿床中的金属含量和比值已预先被输入的岩浆流体成分所确定。结合前人对单一斑岩型铜、钼矿床，单一脉状铅锌银矿床的研究成果可知，钼铅锌银系统的金属分带可能受控于成矿物质从热液流体中的依次沉淀(Audétat et al., 2000)，其触发机制主要包括：(1)减压所致的流体不混溶(Rusk et al., 2008；Landtwing et al., 2010；Allan et al., 2011)；(2)流体降温(Klemm et al., 2007)；(3)流体混合(Cooke et al., 2011；Song et al., 2019；Li et al., 2019)；和(4)水岩反应(Hemley and Hunt, 1992; Cooke and Simmons, 2000)等。(1)流体不混溶现象在斑岩矿床中常被观察到，部分学者认为该过程导致了钼沉淀(Li et al., 2012；Ni et al., 2015)，但也有部分学者认为流体不混溶无法导致整个系统的变化，因而不会触发金属沉淀，但可促进钼在卤水中的预富集(Audétat and Li, 2017)。因此，流体不混溶现象与金属沉淀的关系仍需进一步厘定。(2)流体冷却可以造成钼溶解度下降，驱动钼沉淀(Ulrich and Mavrogenes, 2008)，Questa斑岩钼矿的研究结果支持这一观点，气液相分离后成矿流体温度从420℃降低到360℃，在不到100℃的温度区间内，沉淀了99%的金属钼(Klemm et al., 2008)。(3)大气水加入并与岩浆热液流体混合所导致的流体温度下降可能是控制岔路口矿床大量辉钼矿的集中沉淀的关键因素(Li et al., 2019)。(4)沙让斑岩钼矿利用H-O同位素模拟水岩反应过程，认为成矿流体与围岩的相互作用，可能控制着钼的沉淀(赵俊兴，2013)。此外，Bingham Canyon斑岩铜-钼-金矿床时空上铜和钼两种金属的分离，被认为受控于成矿流体性质的改变，早期铜阶段成矿流体较氧化且中性，而晚期钼阶段成矿流体则更还原且较酸性(Seo et al., 2012)，磁铁矿等氧化性矿物的沉淀可导致成矿流体氧逸度的下降进而引发金属的沉淀(Sun et al., 2004, 2013；Liang et al., 2009)。因此酸碱度和氧化还原态等物理化学条件的变化，可能也是控制钼沉淀的重要因素。
初始成矿流体中通常具有较高的氯浓度，此时Zn、Pb、Ag等元素以氯化物形式存在于热液流体中(Ruaya and Seward, 1986；Mibe et al., 2009；Tagirov and Seward, 2010)。流体温度的降低，可导致Zn-Cl等络合物稳定性降低而沉淀出金属元素。Kostova et al.(2004)通过测定单个流体包裹体中金属的浓度，证明保加利亚Madan的多金属脉状矿床的Pb和Zn，在一温度范围内随着冷却沉淀，金属含量剧烈降低。此外，大气水的混入稀释流体中氯的浓度，也都会导致金属的沉淀(Hemley and Hunt, 1992；Seward and Barnes, 1997)。而水岩反应过程或者其他高pH值的溶体的混入，会导致流体pH值的增大，导致Zn在流体中的络合物以Zn-Cl为主转变为Zn(HS)20和Zn(HS)3-络合物为主(Kouzmanov and Pokrovski, 2012)，由于Zn-Cl络合物的溶解度更高，络合物种类的转变也同样会致使金属大量沉淀。
Pb、Zn、Ag等金属元素能比Mo在更低的温度下保持溶解状态(Wood et al., 1987；Hemley et al., 1992)。从Mo沉淀至Pb、Zn、Ag等元素沉淀，其温度区间具有连续降低的趋势，说明金属元素的分带，受控于流体降温过程。此外，前已述及，水岩反应过程及大气水混合作用对于Mo、Pb、Zn、Ag等元素的沉淀也具有控制作用，因此空间上Mo、Pb、Zn、Ag的分带，可能受控于流体演化过程中，各种地质作用的综合叠加效应。另外，由于岩浆热液流体可能并未包含足够的硫来沉淀所有金属元素(Audétat et al., 2000)，硫的浓度和主要的亲铜元素(Cu，Fe)通常在同一数量级上(Seo et al., 2012)，因此不同金属之间对于硫的竞争作用，可能对于元素分带也起了重要作用。
9 成矿系统的勘查指标通过分析同一成矿系统内斑岩钼矿与脉状铅锌银矿的特征、关联性及勘查历史，本文重点分析该成矿系统勘查工作的指示依据，尤其是借助已查明的浅部脉状铅锌银矿，来寻找指示深部斑岩钼矿存在与否的勘查线索。以岔路口钼铅锌银矿勘查工作(孟昭君等，2011)为例，该矿床首先进行地球化学勘查发现Mo、Zn、Pb、Ag等元素异常，浓集中心明显且分带好，进一步实施地球物理测量，表明河东区激电中梯为低阻高极化异常、高精度磁法负磁异常，经探矿工程验证，槽探揭露出浅部脉状铅锌银矿体；向深部验证过程中，钻探揭露出规律性的斑岩型矿床蚀变分带特征且钼品位较高，通过调整勘查思路，成功探获深部超大型斑岩钼矿床。此外，其他典型钼铅锌银成矿系统例如沙坪沟(张怀东，2018)、千鹅冲(李法岭，2011)、东沟(王令全等，2014)、永定新村(韩胜康，2008)等矿床的勘查发现过程(表 5)，也均包括化探研究揭示Mo、Pb、Zn、Ag等元素浓集和套合、物探资料研判、岩浆岩成矿专属性、斑岩成矿理论、指示性矿物、构造控矿机制等共性特点和步骤。
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表 5 典型斑岩钼-脉状铅锌银成矿系统的主要勘查过程 Table 5 Summaries of exploration history of typical porphyry Mo-vein-style Pb-Zn-Ag systems |
通过分析多个矿床实例的地球化学和地球物理勘查过程(表 5)，构造、岩相特征(表 6)，且结合前述该成矿系统的主要地质、地球化学特征及研究成果，本文总结出可能存在钼铅锌银成矿系统的若干地球化学-地球物理-地质特征指标(表 7)如下：(1)化探结果中Mo、Pb、Zn、Ag等元素浓度高且套合好；(2)物探资料判断深部存在岩体，且显示面状夹线状的激电异常；(3)存在一些浅部优势方位的构造带，例如次级断裂等，深部为面状应力均一体；(4)通常存在高分异的花岗质岩株、岩脉及相关的同期火山岩；(5)热液蚀变自浅向深具有向高温蚀变矿物变化的趋势；(6)可能存在萤石等指示矿物；(7)可能存在辉钼矿-闪锌矿复合脉体；(8)浅部硫化物具有高Mo含量、高Mo/Ag-Bi/Sb和Mo/Pb-Sn/Sb比值(金露英等，2015)，辉钼矿微量元素中具有较高的Pb和Zn含量(Ren et al., 2018b)。
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表 6 典型斑岩钼矿-脉状铅锌银成矿系统和仅有斑岩钼矿实例中同期岩浆活动和构造因素总结 Table 6 Summaries of syn-ore magmatism and tectonic activities in the selected porphyry Mo-vein-style Pb-Zn-Ag systems and Mo-only systems |
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表 7 典型斑岩钼矿、脉状铅锌银矿床和钼铅锌银成矿系统的若干地球化学-地球物理-地质指标 Table 7 Summaries of proposed geochemical, geophysical and geological indicators in the exploration of porphyry Mo deposits, vein-style Pb-Zn-Ag deposits and porphyry Mo-vein-style Pb-Zn-Ag systems |
应用上述提出的指标，当实际勘查中已发现脉状铅锌银矿化，且经综合分析确定目标为寻找同一成矿系统的斑岩钼矿床时，本文建议可从以下方面进一步核查：(1)研究化探结果揭示的Mo与Pb、Zn、Ag、Sb等元素的套合和同心分布特征，分析元素浓度的变化方向；(2)研究物探结果揭示的深部异常体位置，判断岩体存在的实际位置；(3)检查矿床构造特征，即断裂构造和褶皱的构造几何学、运动学和动力学特征，查明控矿构造，研究铅锌银矿化与钼矿化因构造所可能导致的错动或剥蚀情况；(4)研究已揭示的蚀变类型及分带特征；(5)检查辉钼矿-闪锌矿-方铅矿复合脉体的存在情况；(6)分析浅部硫化物的微量元素特征。
10 成矿系统形成的若干因素斑岩钼-热液脉状铅锌银成矿系统虽已引起越来越多的关注，但两类矿化的成因联系，两者的共生和分离要素研究尚处于起步阶段，综合前文已述的单一斑岩钼矿、单一脉状铅锌银矿、斑岩钼-热液脉状铅锌银系统的基本特征，本文对于成矿系统形成的促进因素和保存条件的若干要素初步提出以下考量。
(1) 高分异、高演化、高氟的花岗质岩浆。形成斑岩钼矿的岩浆多为过铝质中酸性-酸性的钙碱性岩浆或碱性岩浆(Westra and Keith, 1981；Carten et al., 1993)，与铅锌银矿化相关的岩浆性质多为中酸性的花岗质岩浆，与钼铅锌银成矿系统相关的则多为高硅高碱高钾高分异的钙碱性花岗质岩石。因此，演化程度较高的酸性花岗质岩浆可能与该系统更密切相关。同时，大部分钼铅锌银成矿系统的岩浆-流体具有高氟特征，例如普遍产出萤石及富氟云母等矿物、岩体具有较高氟含量等(例岔路口矿床，沙坪沟等)。氟元素可起源于与钼元素一致的源区，前人研究发现氟元素来源，包括裂谷作用有关的软流圈地幔(Partey et al., 2009)，碱性岩浆或花岗质岩石的熔融(Van Alstine，1976；Sallet et al., 2005；Agangi et al., 2010)，以及富氟矿物例如磷灰石、角闪石、金云母等矿物熔融(Van Alstine，1976；McLemore et al., 1998)等。氟在岩浆结晶、流体出溶及元素运输过程中起到了重要作用。在岩浆结晶阶段，氟可以降低固相线温度和熔体的粘度/密度(Manning，1981；Webster et al., 1987；Wyllie and Tuttle, 1961)。在岩浆-热液过渡阶段，Chang and Meinert(2004)对Empire铜锌矽卡岩的研究发现，氟降低了熔体的固相线温度，进而改变了热液流体出溶的时间、温度及持续时长，高氟含量所致的低流体出溶温度，促进了近源锌矿化的形成。熔体中氟含量高，还可促进出溶流体中包含更多水和氯等这些利于金属运移的配位剂(Holtz et al., 1993；Seward and Barnes, 1997；Webster，1997；Webster and Rebbert, 1998；Wood and Samson, 1998)。因此，较高的氟含量对于钼铅锌银系统出溶流体的元素预富集、延长出溶时长、降低出溶温度，都可能起到积极的影响。
(2) 具有活跃的岩浆-热液系统。流体出溶过程中的大规模岩浆-热液系统，其成矿元素和挥发分元素高效对流有助于大规模矿化形成(例如沙坪沟，Wang et al., 2014)，之后流体演化过程中流体大尺度迁移并萃取围岩中的成矿物质(毛景文等，2009)，可能更有利于钼铅锌银成矿系统发育。
(3) 具有充足的成矿元素供给。斑岩型矿化的形成，通常需要大量的金属元素及成矿熔体(Hedenquist et al., 1998)。例如形成Questa矿床钼储量0.24Mt，至少需要60Gt或25km3的钼含量为4×10-6的熔体(Klemm et al., 2008)；沙坪沟矿床钼资源量2.43Mt，至少需要500km3的岩浆贡献足量钼(Wang et al., 2014)。脉状铅锌银矿化的形成，也需从成矿岩浆中或者从围岩地层中萃取大量成矿元素(Rice et al., 2007；Subías et al., 2010)。因此足够的岩浆补给量或高成矿元素的地层单元将提供足量的钼及铅锌银元素，是钼铅锌银成矿系统形成的先决条件。而对于硫含量，前人对流体中成矿元素含量的微区分析可知，流体中也常具有较高的铅锌含量且甚至高于钼元素含量，例如Questa钼矿流体中Mo含量为6×10-6~90×10-6，Zn含量为340×10-6~1900×10-6 (Klemm et al., 2008)；Bingham铜钼金矿床流体中Cu含量为560×10-6~10000×10-6，Mo含量为7×10-6~470×10-6，Zn含量为2100×10-6~5500×10-6 (Seo et al., 2012)。然而，即使成矿流体中具有大量金属元素，受限于是否具有足量硫元素及不同金属之间对于硫的竞争作用，成矿流体中的金属元素并不能全部沉淀(Audétat et al., 2000；Seo et al., 2012)。因此在具有足量钼铅锌银元素供给的情况下，金属沉淀阶段是否有足量的硫也是形成成矿系统的关键。
(4) 具有适宜的构造条件(包括同期火山机构发育或同期岩体侵位可能有利于成矿系统形成)。斑岩型矿床通常与区域性构造相关(Sinclair，2007)，例如北美西部Rio Grandelie裂谷系统产出一系列斑岩钼矿床，脉状矿化的发育则常与断裂的发育密切相关。因此次级构造交汇及断裂构造更发育的部位，可提供容矿空间，更适宜成矿系统发育(秦克章等，1990；秦克章，1998)。综合多个典型矿床钼铅锌银成矿系统特征可知，多数成矿系统发育同期火山机构或多期侵入体(表 6)。Sillitoe(1994)根据对斑岩铜矿-高硫型浅成低温金-银矿研究，认为同成矿期岩体侵位或火山热液系统减弱等导致的扇形坍塌，会令热液系统在1Ma的生命周期内古地表下降1km，引起大气水大量进入岩浆环境并造成流体压力下降，最终有助于形成斑岩型矿化与浅成低温金银或者贱金属矿化的套合。
(5) 较好的保存条件。矿床形成后可能会经受后期构造改造、错动、倾斜或者剥蚀破坏等，例如Ann-Mason斑岩铜矿受后期改造，矿床向西倾斜了约90°，令该矿床古深度1~6km的蚀变-矿化特征出露于近地表(Dilles and Einaudi, 1992)，其他例如Robinson斑岩铜金矿等多个矿床形成后倾斜了至少约50°，影响古垂向深度超过3km(Seedorff et al., 2005)，新疆包古图斑岩铜矿形成后曾经历了约8km的抬升剥蚀过程(Li et al., 2014a)。因此斑岩钼铅锌银成矿系统形成后，如受后期构造影响也可能导致斑岩钼或者铅锌银矿化倾斜、被剥蚀或错动，相对较小的构造改造才能令完整的成矿系统得以保存且识别。
11 存在问题及研究展望(1) 为了确切地建立典型斑岩钼-热液脉状铅锌银系统，铅锌银矿化形成时限的精确厘定是非常重要的工作。目前对铅锌成矿年龄多用闪锌矿-黄铁矿Rb-Sr/Re-Os同位素(Li et al., 2015；Liu et al., 2019；Tang et al., 2019)、绢云母Ar-Ar同位素(范海洋等，2018)、萤石-方解石Sm-Nd同位素(Xu et al., 2015；Walter et al., 2018)进行定年。其中，硫化物Rb-Sr等时线年龄准确与否，需要可靠的数据验证硫化物形成时是否同位素高度均一且在相对封闭系统中演化(Wan et al., 2009)，而闪锌矿和黄铁矿Re-Os等时线年龄通常得到较为混乱的年龄结果，往往需要应用LA-ICP-MS面扫描技术等分辨测试矿物的Re-Mo的分布状态，进而评估硫化物Re-Os年龄是否准确(Hnatyshin et al., 2020)。特别是在脉状铅锌银矿床中，硫化物和脉石矿物经常显示多期环带结构，需要利用原位技术分辨矿物的不同期次及元素的分布状态，进而获得该类型铅锌银矿相对准确的成矿年龄。
(2) 目前虽有少量Climax型斑岩钼矿中流体组成被揭示(Audétat et al., 2008；Klemm et al., 2008；Audétat and Li, 2017)，斑岩钼-热液脉状铅锌银成矿系统的初始流体成矿元素、硫含量和相关配位剂元素的含量尚未得到准确限定，其与单一斑岩钼矿化甚至其他斑岩矿床系统的初始流体在元素含量上有何差异尚未得知。在限定的钼铅锌银体系中，确定各阶段流体的元素含量组成(特别是钼铅锌复合脉体)，将有助于揭示斑岩成矿系统钼铅锌银成矿效率和矿质沉淀的关键控制因素(Kouzmanov and Pokrovski, 2012)。
(3) 热液矿物的空间分布、结构和成分的研究能够揭示成矿流体的组成、来源、演化和矿质沉淀过程(Seedorff et al., 2005；Wilson et al., 2007)，并为实际勘查工作提供强有力的依据(例如辉钼矿，Ciobanu et al., 2013；明矾石，Chang et al., 2011；绿帘石，Cooke et al., 2014；绿泥石，Wilkinson et al., 2015)。而上述研究多数为斑岩铜金矿床和浅成低温热液矿床，典型斑岩钼-热液脉状铅锌银矿系统指示性矿物研究虽有尝试(例如岔路口硫化物，金露英等，2015；沙坪沟辉钼矿，Ren et al., 2018b)，但仍需从脉石矿物和矿石矿物多个角度厘定钼铅锌银矿成矿系统的矿物学指示标志，以期对成矿系统的勘查指标建立提供依据。
(4) 由于钼铅锌银成矿系统近几年才被识别，尚未对典型实例进行全面深入剖析，研究还很薄弱。该系统的岩浆过程，地幔和围岩物质的参与程度及与成矿的关系；硫元素、氟、氯等配位剂元素在流体出溶-演化过程中的行为和影响作用；同期火山作用及构造作用的影响等多方面的精细成矿过程等需要更多的研究实例来支持。此外，该系统与单一斑岩钼矿、单一热液脉状铅锌银矿的差异及共生、分离因素也需进一步研究。
12 结语斑岩钼-热液脉状铅锌银成矿系统研究的重要意义，在于深入研究斑岩钼矿床与热液脉状铅锌银矿床，乃至浅成低温银矿床的成因联系，厘清岩浆-流体演化过程、蚀变-矿化过程、金属共生及分离机制，有助于丰富钼铅锌银矿系统的成矿理论。我国东部存在大量斑岩钼矿床(矿化点)和脉状铅锌(银)矿床(矿化点)，建立斑岩钼-脉状铅锌银矿化的成矿模式和找矿标志，将有助于推进钼铅锌银资源的勘查工作。本文总结了该成矿系统勘探过程中几个重要因素，包括指示性矿物与脉体组合、热液蚀变特征、岩浆岩属性、构造条件、物探-化探特征和浅部硫化物特征等。下一步将搜集更多相关矿床的资料进行对比分析和验证，结合典型成矿系统中指示性矿物的相关研究，检验这些找矿标志是否具有普适性和推广性，以期对浅部铅锌银矿之下深部斑岩钼矿的找矿工作，以及已知斑岩钼矿周边热液脉状铅锌银矿的找矿工作有所帮助。
致谢 成文过程得到了黑龙江有色地勘局706队孟昭君高工、中国科学院地质与地球物理研究所曹明坚研究员、中国科学院青藏高原研究所李金祥研究员的帮助、指导和启发，得到了三位审稿人的宝贵修改意见和建议，得到了期刊编辑的精心修改，使文章得以完善。在此一并致以诚挚的谢意！
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