豫西雷门沟钼矿区西段隐爆角砾岩地球化学特征及地质意义*

章传飞 周炳龙 夏明哲 陈丹利 星东

1. 河南省地质矿产勘查开发局第三地质勘查院，郑州 450001

2. 河南省金属矿产深孔钻探工程技术研究中心，郑州 450001

3. 长安大学地球科学与资源学院，西安 710054

东秦岭钼矿带位于华北克拉通南缘，是我国最大的钼多金属成矿带，仅次于美国Climax-Henderson斑岩型钼矿带(李永峰等, 2005; 魏庆国等, 2009)。东秦岭钼金属储量约占全国钼总储量的66%(张正伟等, 2001; Maoetal., 2011)，其中以斑岩型钼矿为主，如金堆城、南泥湖、三道庄、雷门沟等超大型钼矿床(图1a)(Steinetal., 1997; 李永峰等, 2003; 叶会寿等, 2006)。雷门沟钼矿床作为自然资源部找矿突破战略行动优秀找矿成果和中国地质学会评选的2017年度十大地质找矿成果之一(河南省地质矿产勘查开发局第三地质勘查院, 2016(1)河南省地质矿产勘查开发局第三地质勘查院. 2016. 河南省嵩县雷门沟矿区中西段钼矿详查报告)，其矿床地质特征、成矿年代、成矿流体和物质来源以及矿床成因等科学问题备受关注(张正伟等, 2001; 卢欣祥等, 2002; 陈小丹等, 2011, 2012; 李永峰等, 2006; Chenetal., 2014; 曹晶等, 2016; Caoetal., 2017, 2018)。雷门沟钼矿的成矿岩体主要由隐爆角砾岩和部分花岗斑岩、二长花岗斑岩组成(图1b)，隐爆角砾岩分布在花岗斑岩和二长花岗斑岩周围。北美的58个斑岩型矿床中有70%成矿岩体内发育隐爆角砾岩(翟裕生等, 2011)，显示隐爆角砾岩在成矿中的重要作用及指示意义。通常隐爆作用形成的角砾岩为成矿流体提供良好的容矿和导矿空间，其成岩过程往往也伴随着成矿过程(McCallum, 1985; 林书平等, 2012; 陈云杰等, 2012; 高荣臻等, 2014)。随着发现越来越多与隐爆作用有关的金属矿床，隐爆角砾岩也成为地质勘探的热点，而且在岩浆热液型金矿/浅成热液金矿床(如祁雨沟)和斑岩型钼铜矿床找矿过程中，往往把隐爆角砾岩作为重要的找矿标志(Sillitoeetal., 2003; 王忠, 2004; 励音骐等, 2010; 高荣臻等, 2014)。由此可见，针对隐爆角砾岩开展深入研究，对指导找矿、探究成矿规律等极为必要。因此，本文选择雷门沟隐爆角砾岩为研究对象，通过对其岩相学、地球化学研究，探讨隐爆角砾岩的成岩环境以及与成矿的关系，希望对今后斑岩钼矿床的找矿勘查有所指导。

1 区域地质背景

雷门沟钼矿床位于华北克拉通南缘秦岭造山带后陆逆冲断裂褶皱带(张正伟等, 2001)，其北部以三宝断裂为界与华北克拉通相邻，南部以黑沟-栾川断裂为界与北秦岭中-新元古界宽坪群接触(图1a)。研究区内地层具有克拉通结晶基底、盖层双重结构。结晶基底由新太古界太华群TTG(英云闪长岩-奥长花岗岩-花岗闪长岩)片麻岩和斜长角闪岩组成(胡受奚等, 1997; 罗铮娴等, 2018; Jiaetal., 2019)，盖层主要由元古界熊耳群、官道口群和栾川群等组成(河南省地质矿产局, 1989)。区内燕山期花岗质岩浆活动广泛发育，包括正长斑岩脉、石英斑岩脉、二长花岗斑岩脉、花岗斑岩岩株及隐爆角砾岩，其中花岗斑岩的LA-ICP-MS锆石U-Pb年龄为131±1Ma(Caoetal., 2018)，石英斑岩脉的LA-ICP-MS锆石U-Pb年龄为127±1Ma(陈小丹等, 2011)。主要以两种形式产出，一类为大岩基，如花山、五丈山、娘娘山、文峪、华山、老牛山等(图1a)；另一类为小的斑岩体，如雷门沟、南泥湖、金堆城等(图1a)，这些小斑岩体与钼等多金属矿化关系密切，呈现“小岩体成大矿”的特点(汤中立和李小虎, 2006; 王晓霞等, 2011)，其成矿年龄为132±2Ma(ICP-MS辉钼矿Re-Os同位素年龄，李永峰等, 2006)。区内地层、岩浆岩和构造等均受南坡岭-花山背斜控制，呈近东西向展布。背斜轴面倾向195°～220°，倾角26°～38°。核部出露岩石为混合岩化斜长角闪岩，翼部出露为黑云母角闪斜长片麻岩。

雷门沟钼矿床西侧发育花山和五丈山岩基(图1a)。花山花岗岩基位于矿区北西侧约6km，出露面积超过300km2，呈不规则状侵位于太华群片麻岩中，局部侵入熊耳群中(范宏瑞等, 1994)，其成岩年龄为132～131Ma(Maoetal., 2010)。五丈山花岗岩基位于矿区西南部，出露面积约58km2，区域上呈北西-南东向延伸，其成岩年龄为157±1Ma(Maoetal., 2010)。围绕花山岩基、五丈山岩基普遍发育一系列小型花岗岩类岩株、岩脉以及与其有成因联系的隐爆角砾岩体(图1b)，如雷门沟、祁雨沟等(张元厚, 2006; 刘征华, 2010)。

图1 雷门沟钼矿大地构造位置(a, 据Mao et al., 2010)及地质简图(b, 据李永峰等, 2006)Fig.1 Simplified sketch map and geotectonic location showing distribution for the Leimengou Mo deposit (a, after Mao et al., 2010; b, after Li et al., 2006)

雷门沟矿区内共圈定出工业矿体19个，钼金属资源量63.64万t，其中2号、40号矿体为主矿体。雷门沟2号矿体规模大、呈长圆近环状，位于花岗岩体和太华群片麻岩系的内外接触带附近和隐爆角砾岩中(图2)，Mo平均品位为0.079%，金属量近61万t。40号矿体位于2号主矿体下部，呈薄层状、透镜状产于花岗斑岩和二长花岗斑岩体内，Mo平均品位为0.096%，金属量近0.9万t(河南省地质矿产勘查开发局第三地质勘查院, 2016)。

图2 雷门沟钼矿西段隐爆角砾岩中2号矿体Ⅰ-Ⅰ′和Ⅱ-Ⅱ′勘探线剖面图Fig.2 Geological sections along No.Ⅰ-Ⅰ′ and Ⅱ-Ⅱ′ exploration lines of the No.2 ore body in the western Leimengou Mo deposit

2 隐爆角砾岩岩体地质和岩相学

2.1 隐爆角砾岩岩体地质

隐爆角砾岩分布在花岗斑岩和二长花岗斑岩周围，岩体西侧出露面积最大，其展布方向和分布范围严格受岩体控制(图1b)。东部隐爆角砾岩呈孤岛状、半圆状、椭圆状、透镜状，大小不一，一般数百米，宽数十米。西部隐爆角砾岩长1500m，宽约500m，呈拳头状分布在岩体西侧，剖面上多呈筒状、漏斗状分布，少量呈树枝状分布(严正富等, 1986)。根据隐爆角砾岩在岩体空间内的产出位置，可划分为顶盖角砾岩、边部角砾岩和内部角砾岩(刘征华, 2010)。本文研究对象为矿区西部的顶盖角砾岩，出露较好，呈灰褐色，岩石碎裂明显(图3a, b)。角砾岩的北界陡立，南界向内倾，倾角50°，延伸约200～400m，局部有二长花岗斑岩侵入。在角砾岩核心部位，角砾大小多为数厘米到数十厘米，次圆状-次棱角状；向边部，角砾逐渐变大，达数十厘米至数米，个别可达数十米，局部与围岩界线不清晰(刘征华, 2010)。

图3 雷门沟西段钼矿区隐爆角砾岩野外露头(a、b)、手标本(c、d)及显微照片(e、f)(a)样品采集位置，废弃采矿洞；(b)隐爆角砾岩野外露头；(c)含脉状辉钼矿角砾岩；(d)浸染状辉钼矿角砾岩；(e)角砾-胶结物接触部显微照片(单偏光)；(f)胶结物中脉状辉钼矿(单偏光)Fig.3 Field outcrops (a, b), hand specimens (c, d) and micrographs (e, f) of cryptoexplosive breccia in the western part of the Leimengou molybdenum ore area(a) sample collection location, abandoned mining hole; (b) the outcrop of cryptoexplosive breccia; (c) the breccia containing vein-like molybdenite; (d) the breccia containing disseminated molybdenite; (e) micrograph of breccia-cement contact (single polarized light); (f) vein molybdenite (single polarized light)

2.2 岩相学

隐爆角砾岩颜色变化较大，为灰色-浅肉红色，主要由角砾及胶结物组成，角砾成分主要为太华群片麻岩、混合岩以及已固结的花岗斑岩，呈次圆状-次棱角状，砾径变化较大(图3c, d)，从数厘米至数米，个别可达数十米。胶结物多为花岗岩类岩石(图3c, e)，局部可见岩粉、岩屑及少量热液蚀变矿物(刘征华, 2010)。

隐爆角砾岩中普遍具有钼矿化(图3e, f)。隐爆角砾岩型矿石呈深灰色，具有自形-半自形粒状结构、他形粒状结构、鳞片状结构、交代残余结构和包含结构，构造有脉状、浸染状、角砾状和块状。主要的矿石矿物为辉钼矿，次为黄铜矿、黄铁矿、磁铁矿等；脉石矿物有钾长石、石英、斜长石、黑云母、绿泥石、绿帘石等，含少量的绢云母、萤石、硬石膏等。

3 样品采集与分析方法

样品采集位置见图1b(坐标：34°12′17.8″N、11°54′39.0″E)，为废弃的采矿洞中心及其周边，洞内出露岩石主要为(含矿)隐爆角砾岩。为了更全面、准确的反映隐爆角砾岩地球化学特征，利用微钻技术在不同部位分别取出角砾(LMG18-1、LMG18-4、LMG18-6)和胶结物(LMG18-2、LMG18-5)进行分析。主量、微量及稀土元素分析测试工作在广州市拓岩检测技术有限公司完成，主量元素采用测试仪器3080E型X-荧光光谱仪，精度优于1%；微量元素采用电感耦合等离子质谱仪(LA-ICP-MS)进行分析，精度高于5%。隐爆角砾岩中角砾和胶结物的主、微量元素和稀土元素分析结果见表1。

表1 雷门沟钼矿隐爆角砾岩中角砾和胶结物主量元素(wt%)和微量元素(×10-6)分析结果Table 1 Major (wt%) and trace (×10-6) elements of the breccia and cement in the Leimengou cryptoexplosive breccia

4 讨论

4.1 主量元素特征

隐爆角砾岩中角砾和胶结物主量元素见表1。角砾SiO2含量较低，为56.61%～64.66%，为中酸性岩类，胶结物SiO2含量较高，为71.62%～72.47%，为酸性岩类；角砾Al2O3含量为11.46%～17.67%，胶结物Al2O3含量为10.86%～12.35%；角砾的全碱含量Na2O+K2O为7.27%～12.90%，平均值为9.57%，具有富碱的特征，且K2O含量高于Na2O含量，K2O/Na2O比值为1.19～25.12，大于0.5，属钾质系列岩石；A/CNK比值为1.06～1.14，显示铝过饱和；里特曼指数σ为2.44～10.97，平均值为6.26，属钙碱性-碱性系列。胶结物的全碱含量Na2O+K2O为8.32%～9.00%，具有富碱的特征，且K2O含量高于Na2O含量，K2O/Na2O比值为3.50～6.21，大于0.5，属钾质系列岩石；A/CNK比值为1.00～1.02，显示铝弱过饱和；里特曼指数σ为2.35～2.83。

在硅碱图解中(图4a)，角砾和胶结物大部分岩石落入碱性系列，岩石类型变化较大。在AFM图解中(图4b)，角砾表现出富铁的趋势，属于钙碱性岩石系列，而胶结物落入拉斑系列；在SiO2-K2O图解中(图4c)，角砾和胶结物全部落入钾玄岩系列中；在A/CNK-A/NK图解中(图4d)，岩石角砾均位于过铝质系列中，胶结物位于准铝质-过铝质分界带。

图4 雷门沟隐爆角砾岩角砾和胶结物成分TAS图解(a,底图据Middlemost, 1994)、AFM图解(b,底图据Irvine and Baragar, 1971)、SiO2-K2O图解(c,底图据Rickwood, 1989)和A/CNK-A/NK图解(d,底图据Rickwood, 1989)Ir-碱性与亚碱性分界线(Irvine and Baragar, 1971).数据来源：雷门沟矿区花岗斑岩、二长花岗斑岩据Cao et al. (2018)；花山岩体据聂政融等(2015)；太华群片麻岩据Jia et al. (2019)；图5和图6数据来源同此图Fig.4 TAS (a, after Middlemost, 1994), AFM (b, after Irvine and Baragar, 1971), SiO2 vs. K2O (c, after Rickwood, 1989) and A/CNK vs. A/NK (d, after Rickwood, 1989) diagrams of the breccia and cement in the Leimengou cryptoexplosive brecciaIr: Alkaline and Subalkaline dividing line (Irvine and Baragar, 1971). Data sources: granite porphyry and monzonite porphyry in Leimenggou from Cao et al. (2018); the Huashan granite from Nie et al. (2015); Gneiss of the Taihua Group from Jia et al. (2019); also in Fig.5 and Fig.6

4.2 稀土微量元素特征

隐爆角砾岩中角砾和胶结物的稀土和微量元素含量见表1。角砾稀土元素总量∑REE变化较大，为69.50×10-6～1408×10-6，平均值为538×10-6，LREE/HREE比值变化较大，为5.09～17.58，说明轻、重稀土元素分异明显；(La/Yb)N值为4.49～28.64，说明轻稀土元素呈现出不同程度的右倾配分模式；(La/Sm)N值为2.80～5.54，(Gd/Yb)N值为1.21～3.31，δEu为0.36～0.71，显示强烈的铕负异常。胶结物的稀土元素总量∑REE为395.5×10-6～584.2×10-6，LREE/HREE比值为12.95～17.43，显示强烈的轻重稀土元素分馏；(La/Yb)N值为19.70～33.60，说明轻稀土元素呈现出强烈富集的右倾配分模式；(La/Sm)N值为5.77～7.08，(Gd/Yb)N值为2.49～3.30，δEu为0.37～0.39，显示强烈的铕负异常。

隐爆角砾岩中角砾和胶结物球粒陨石标准化稀土元素配分曲线基本一致(图5a)。所有岩石均具有明显的负铕异常，这与新太古界太华群片麻岩、矿区内花岗斑岩、花山岩体的稀土元素配分曲线是一致的(图5a, c)，但后两者稀土元素总量较低，铕负异常不明显(图5c)。从样品的原始地幔标准化微量元素蛛网图上(图5b, d)可以看出，隐爆角砾岩角砾和胶结物与太华群片麻岩、矿区内花岗斑岩、花山岩体具有相似的微量元素配分模式，表现出富集大离子亲石元素(Cs、Rb、Ba、K、Pb)，明显亏损高场强元素(Nb、Ta、Ti)。其中一件角砾样品(LMG18-5)除明显亏损Zr、Hf外，与其他样品的元素特征基本一致。结合稀土元素球配分曲线特征，隐爆角砾岩中角砾大部分可能来自于新太古界太华群片麻岩。

图5 雷门沟钼矿隐爆角砾岩及相关岩石球粒陨石标准化稀土元素配分图(a、c)及原始地幔标准化微量元素蛛网图(b、d)(标准化值据Sun and McDonough, 1989)Fig.5 Chondrite-normalized REE patterns (a, c) and primitive mantle-normalized trace element spider diagrams (b, d) for the Leimengou cryptoexplosive breccia and related rocks (normalization values after Sun and McDonough, 1989)

4.3 成岩环境

隐爆角砾岩中胶结物全碱含量(Na2O+K2O)为8.32%～9.00%，K2O/Na2O比值为3.50～6.21，A/CNK比值为1.00～1.02，里特曼指数(σ)介于2.35～2.83，属于过铝质高钾钙碱性-碱性岩石系列。过铝质岩石多出现在碰撞造山带，而高钾钙碱性-碱性岩石一般代表了碰撞造山的结束，开始向板内伸展环境转变(Harrisetal., 1986; 韩宝福, 2007)，这与东秦岭地区中生代晚期花岗岩成岩环境相同(肖娥等, 2012; 曹晶等, 2016; Lietal., 2018)。胶结物明显富集大离子亲石元素(Rb、Cs、K、Ba、Pb)和轻稀土元素LREE，相对亏损高场强元素(Ta、Nb、Ti)，显示具有岛弧环境的特点，或是出现在与地壳混染作用相关的造山后伸展环境(邓晋福等, 2009; 章邦桐等, 2002; 田敬佺等, 2015)。隐爆角砾岩中角砾Y为16.40×10-6～91.30×10-6，TiO2为0.21%～0.60%，Th/Yb比值为0.23～0.61，这与造山后花岗岩和太华群片麻岩非常相似。隐爆角砾岩的胶结物Sr为232×10-6～267×10-6，而Yb为3.16×10-6～3.35×10-6。据张旗等(2006，2008)研究，将该岩石划分为低Sr、高Yb花岗岩，其形成压力通常小于1.0GPa，类似于浙闽型花岗岩。在Rb-(Yb+Ta)图解中，角砾和胶结物全部位于同碰撞花岗岩区(图6a)；在Ta-Yb图解中，除一件角砾样品(LMG18-1)位于板内和大洋脊分界线处，其余样品位于火山弧环境中(图6b)；在Nb-Y图解中，样品位于火山弧-同碰撞和板内环境中(图6c)；在Rb/10-Hf-Ta×3图解中，所有样品位于碰撞背景下花岗岩区(图6d)。判别图显示矿区花岗斑岩和花山岩体形成于同碰撞环境，而太华群片麻岩具有火山弧花岗岩的特点(图6a-d)。由此可知，隐爆角砾岩的成岩环境可能是碰撞后伸展环境。

图6 雷门沟隐爆角砾岩构造环境判别图(a) Rb-(Yb+Ta)图解，(b) Ta-Yb图解，(c) Nb-Y图解(Pearce et al., 1984)；(d) Rb/10-Hf-Ta×3图解(Harris et al., 1986)Fig.6 Discrimination diagrams of tectonic setting for the Leimengou cryptoexplosive breccia(a) Rb vs. (Yb+Ta), (b) Ta vs. Yb and (c) Nb vs. Y diagrams (after Pearce et al., 1984); (d) Rb/10-Hf-Ta×3 diagram (after Harris et al., 1986)

雷门沟钼矿隐爆角砾岩中胶结物与花岗斑岩、二长花岗斑岩紧密伴生，具有相同或相近的地质年龄。雷门沟花岗斑岩形成年龄为136±2Ma(锆石SHRIMP U-Pb年龄，李永峰等, 2006)，二长花岗斑岩年龄为124.0±0.6Ma(锆石LA-ICP-MS U-Pb，陈小丹等, 2011)。毗邻的祁雨沟金矿爆破角砾岩的年龄为～130Ma(132.9±1.5Ma，辉钼矿Re-Os，Wangetal., 2020；132.9±1.4Ma，云母Ar-Ar，Wangetal., 2021)。区域资料表明：扬子克拉通与华北克拉通碰撞汇聚的时间为218～238Ma(李曙光等, 1989)；紧接着是陆内造山阶段，结束于侏罗纪(陈衍景和富士谷, 1992)。在侏罗纪晚期和白垩纪早期，区域构造体制开始变化，应力场从近N-S变为E-W，标志着太平洋构造演化阶段(任纪舜, 1991)。在这个阶段，华北克拉通南缘进入拉张构造环境，以燕山期岩浆强烈活动为特征。由此说明雷门沟隐爆角砾岩也形成于碰撞后伸展阶段(Maoetal., 2008)。

4.4 隐爆角砾岩成因与成矿

华北克拉通南缘在燕山期处于碰撞后伸展体制，形成了大量的断裂构造及岩石裂隙，为隐爆角砾岩的形成提供了良好的地质条件，而且在此期间岩浆热液活动频繁，带来足够多的成矿物质。研究发现东秦岭中酸性小斑岩体及其附近的隐爆角砾岩的胶结物形成深度大于30km的下地壳中(王晓霞等, 1986)。因此推测，幔源或地壳深部的岩浆热液沿断裂构造上升，并在其顶部和周围聚集了大量气体和挥发性组分，由于近东西向断裂构造活动，岩浆热液骤然减压，在封闭或半封闭条件下发生了隐爆作用，使得岩浆顶部/边部的片麻岩、早期固结的花岗岩等破碎并混入岩浆中形成隐爆角砾岩(刘征华, 2010)。Mo是中度不相容亲铜元素，化学性质较活泼，往往以辉钼矿的形式迁移(图3c, f)(孙卫东等, 2015)。由于整个成矿过程是在封闭或半封闭条件下发生的，含矿热液未能挥发，由隐爆作用形成的裂隙和空隙等有利部位很容易就位成矿(McCallum, 1985; 林书平等, 2012; 陈云杰等, 2012; 高荣臻等, 2014)。雷门沟西段新探获的钼矿区具有多期岩浆隐爆作用的特征，在破碎带中常形成了一些Mo矿体，所以，隐爆角砾岩的隐爆作用往往伴随着成矿过程，同时岩浆隐爆作用往往具有多期隐爆及多期成矿的特征(张维根, 1988; McCallum, 1985; 章邦桐等, 2002; 高荣臻等, 2014)。

5 结论

(1)雷门沟西段钼矿区隐爆角砾岩呈筒状分布，具有典型的角砾状构造，角砾大小不一，主要呈次圆状-次棱角状，角砾岩与花岗斑岩-二长花岗斑岩紧密伴生。

(2)雷门沟西段隐爆角砾岩中胶结物和角砾属于过铝质高钾钙碱性岩石系列，胶结物相对富集大离子亲石元素(如K、Rb、Pb)和轻稀土元素，相对亏损高场强元素(如Ti、Ta、Nb)，呈现轻稀土元素富集的右倾式配分模式特征，具有中等负铕异常。

(3)雷门沟西段隐爆角砾岩中胶结物岩石地球化学特征显示其可能形成于碰撞后伸展体制。

(4)雷门沟西段隐爆角砾岩的成岩过程伴随着钼成矿过程。

致谢本次研究岩石主微量元素分析测试得到了广州市拓岩检测技术有限公司的帮助！感谢两位审稿人对本文细致的评阅和中肯的建议。

附表1 辉钼矿中Re的含量与矿床Mo品位数据Appendix Table 1 Re concentrations in molybdenite and Mo grades of porphyry deposits

续附表1Continued Appendix Table 1矿产地矿种组合样品数(n)ReMin(×10-6)ReMax(×10-6)ReAve(×10-6)Mo品位(%)参考文献Michiquillay, CajamarcaCu8127.3735.7494.00.020Marinov,2011Galeno, CajamarcaCu1810.00.020QuestaMo42.00113.068.000.144Berzina et al.,2005;Voudouris et al.,2013Mineral parkCu2250.0290.0270.00.032MajdanpekCu32320355027700.006TongkuangyuCu3172.01280900.00.032KadzharanCu-Au23733.002620245.00.050BorlyCu-Au19250.0550031600.011BoshchekulCu-Au23230.01500825.00.010KounradCu-Au20620.0405015400.010KalmakyrCu-Au20700.0200015000.005ToquepalaCu3387.01496790.00.040ElyCu1250284020200.010Castle DomeCu1200175015500.006EsperanzaCu-Mo90.001800610.00.028MorenciCu-Mo5100.0410011800.095MiamiCu-Mo600.00.010Santa RitaCu5200.01100750.00.008Silver BellCu-Mo18340.0620.0470.00.013Twin ButtesCu-Mo1600.00.023ClimaxMo11.0080.0035.000.240copper creekCu31200420023000.005ChuquicamataCu-Mo3194.0245.0220.00.040CollahuasiCu-Mo2368.0448.0410.00.040El SalvadorCu570.00.010El TenienteCu6182.01154390.00.016EscondidaCu-Au113550.006Los PelambresCu-Mo3450.0820.0600.00.016Erdenetuin-OboCu-Mo3104.0199.0163.70.012ShakhtamaMo-Cu49.0024.0016.750.150AksugCu-Mo1460.00.015ZhirekenMo-Cu712.0057.0029.000.099SoraMo-Cu96.0018.0014.000.058Red BirdMo26.0043.0025.000.065Sinclair et al.,2009carmiMo310.00139.058.000.064cassiar molyMo23.0014.009.000.026lucky shipMo141.000.067storie molyMo315.0022.0020.000.078tidewaterMo213.00109.061.000.060catfaceCu159.000.007AdanacMo48.0022.0012.000.069Ajax WestCu-Au131610.006

续附表1Continued Appendix Table 1矿产地矿种组合样品数(n)ReMin(×10-6)ReMax(×10-6)ReAve(×10-6)Mo品位(%)参考文献BergCu-Mo467.00215.0152.00.031Sinclair et al.,2009BethlehemCu3190.0980.0553.00.005Boss MountainMo749.00157.080.000.074BrendaCu-Mo1295.00145.0115.00.037Bronson SlopeCu-Au1180.00.006Endako 1Mo1215.0067.0035.000.070Endako 2Mo3204.0397.0302.00.070GibraltarCu4238.0750.0443.00.006Glacier Gulch(Davidson)Mo234.0041.0038.000.177GranisleCu4522.0528.0526.00.006HuckleberryCu2247.0258.0253.00.014IngerbelleCu-Au116200.002IslandCopperCu21704186317840.009KemessSouthCu-Au23106460938580.008KitsaultMo257.00102.079.500.115LomexCu1345.00.050MaggieCu-Mo1643.00.029McIntyre-Copper ZoneCu-Au111920.010McLeod LakeCu-Mo1184.00.050Ryan LakeCu-Mo1104.00.039Schaft CreekCu-Mo1590.00.019TominskoeCu110800.004

附表2 斑岩型矿床辉钼矿Re含量与成矿时代数据Appendix Table 2 Re concentrations in molybdenite and ages of porphyry deposits

续附表2Continued Appendix Table 2矿产地矿种组合样品数(n)ReMin(×10-6)ReMax(×10-6)ReAve(×10-6)年龄(Ma)参考文献呼扎盖吐Mo-Cu1222.5180.0刘瑞斌,2016石家湾Mo110.1710.1710.17138.0黄典豪等,1994刘生店Mo615.7118.0816.63169.4王辉等,2011铜坑Mo656.43365.2225.4115.7王少怀和黄宏祥,2015撒岱沟门Mo27.207.507.35142.0代军治,2008曹四夭Mo40.060.090.07130.0聂凤军等,2013纳日贡玛Cu-Mo735.4975.0154.1340.9王召林等,2008石马洞Mo919.9432.5726.03169.3邵建波等,2016太平沟Mo69.9069.1832.31131.0翟德高等,2009鹿鸣Mo519.0125.1022.78183.4孙庆龙等,2014必鲁甘干Mo-Cu467.5685.7374.07237.9李俊建等,2016岔路口Mo81.7088.4828.70147.0聂凤军等,2011长安堡Mo-Cu525.1734.8029.54168.0松权衡等,2016小东沟Mo62.2010.275.56135.5聂凤军等,2007阿林诺尔Mo726.0066.4049.42227.7薛静等,2010金堆城Mo312.9019.7016.13131.0黄典豪等,1994大银尖Mo112.89122.1杨泽强,2007鸡冠山Mo58.1995.6540.92155.0陈伟军等,2010西沙德盖Mo911.0821.1217.04226.4侯万荣等,2010大苏计Mo43.2610.056.15222.5张彤等,2009东沟Mo24.104.264.18115.1Mao et al.,2008东戈壁Mo525.40131.1074.10233.2吴云辉等,2013福安堡Mo59.9415.1311.74166.9李立兴等,2009十二排Mo50.714.512.30151.0王少怀,2013查干花Mo964.50245.7124.9238.6李光耀等,2020沙坪沟Mo52.4110.365.83111.0孟祥金等,2012熊家山Mo50.170.610.45152.0孟祥金等,2007邱埕Mo614.31174.721.94150.1范飞鹏等,2020石门山Mo41.051.671.3081.8陈沐龙等,2015;李孙雄等,2014大庄科Mo513.2027.6619.29137.6刘舒波等,2012砺山Mo913.4120.0318.3191.7王成辉等,2009b赤路Mo54.2816.1710.13106.0张克尧等,2009温泉Mo520.4733.5226.23214.0宋史刚等,2008园珠顶Cu-Mo122.69449.492.04151.0钟立峰等,2010大宝山Cu-Mo530.4676.4762.70163.6向建华等,2018锡坪Mo-Cu40.581.921.0789.9郑伟等,2017

续附表2Continued Appendix Table 2矿产地矿种组合样品数(n)ReMin(×10-6)ReMax(×10-6)ReAve(×10-6)年龄(Ma)参考文献大湾Mo69.1524.8219.17137.0丁海洋,2014木吉村Cu-Mo5163.3409.0289.0144.8申志超等,2015安妥岭Mo553.32104.973.04147.3者萌等,2014大草坪Mo31.1012.606.90140.0代军治,2008雷门沟Mo218.4025.9022.15131.6李永峰等,2006千鹅冲Mo415.4618.5717.40127.8杨梅珍等,2010汤家坪Mo123.9611.946.83113.1杨泽强,2007;Mao et al.,2008天目沟Mo131.99121.6杨泽强,2007多宝山Cu-Mo3303.2567.0469.4506.0赵一鸣等,1997铜山Cu-Mo2497.0822.0659.5506.0赵一鸣等,1997霍吉河Cu-Mo412.0430.9217.39188.0张琳琳等,2014铜山口Cu-Mo2203.6224.3214.0142.9谢桂青等,2006丰山洞Cu-Mo1436.5144.0谢桂青等,2006白鸭山Mo47.2210.909.14100.7陈炜等,2014黄家沟Mo614.7529.1821.76131.3牛志勇等,2017朱砂红Cu40.401.480.80172.6曲焕春等,2015王坞Mo-Cu53.596.387.15134.8戴盼等,2018金竹坪Mo50.170.870.46135.5张家菁等,2009宝山Cu627.96204.7106.1147.7贾丽琼等,2015新台门Mo57.2522.1014.88178.0张遵忠等,2009兰家沟Mo71.5063.47211.7184.6Zeng et al.,2013小狐狸山Mo67.2232.9319.40220.0彭振安等,2011查干德尔斯Mo1553.64211.4140.1241.4蔡明海等,2011乌日尼图Mo-Cu55.2523.3821.97146.5白珏和张可,2013白乃庙Cu-Mo5222.2893.1603.0440.5冯晓曦等,2015乌奴格吐山Cu-Mo6120.5299.4221.0177.4谭钢等,2010车户沟Mo-Cu957.9995.1969.04250.2孟树等,2013八大关Cu-Mo7170.2487.7316.4228.7康永建,2015白土营子Mo-Cu639.6056.6747.43247.0孙燕等,2013劳家沟Mo-Cu524.3871.8754.70235.0Duan et al.,2015敖仑花Mo55.9638.9318.40132.0马星华等,2009毕力赫Cu-Au647.101688745.9272.7卿敏等,2011乌和尔楚鲁图Mo51.6113.258.25158.0俞礽安等,2016鸭子沟Cu-Mo110.373.611.08224.7何书跃等,2009八里坡Mo538.40155.967.67155.0焦建刚等,2009桂林沟Mo692.29193.0143.0197.2张红等,2015

续附表2Continued Appendix Table 2矿产地矿种组合样品数(n)ReMin(×10-6)ReMax(×10-6)ReAve(×10-6)年龄(Ma)参考文献吉如Cu-Mo547.9587.3370.2849.0龚福志等,2008岗讲Cu-Mo12155.9171.1162.913.6杨震等,2017厅宫Cu-Mo7225.7922.7485.816.0李光明等,2005驱龙Cu-Mo6306.71218616.216.0孟祥金等,2003沙让Mo736.1974.2354.1251.0唐菊兴等,2009a玉龙Cu-Mo566.91352.2173.241.6唐菊兴等,2009b多不杂Cu6286.1623.4445.4118.0佘宏全等,2009达巴特Cu-Mo70.150.680.25287.0张作衡等,2006莱历斯高尔Cu-Mo518.5073.5036.80379.9朱明田等,2010土屋-延东Cu-Mo718.261665525.3322.0芮宗瑶等,2002白山Cu-Mo784.04273.6158.3223.2涂其军等,2014马厂箐Mo-Cu734.1061.4049.0635.0王登红等,2004金平铜厂Cu-Mo92.27134.9052.1635.0王登红等,2004铜厂Cu-Mo5416.915711138171.0Guo et al.,2012富家坞Mo-Cu5180.1652.5346.5171.0Guo et al.,2012

附表3 辉钼矿Re含量与成矿岩体平均SiO2含量、分异指数及TiO2和FeOT含量Appendix Table 3 Re concentrations in molybdenite and SiO2 content, DI, TiO2 and FeOT contents for ore-forming porphyries

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