Geology and Genesis of Lead-Zinc Polymetallic Deposits in the Great Xing'an Range
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摘要: 随着近年来找矿工作的不断突破，大兴安岭地区的铅锌多金属矿床在矿化元素组合、矿床时空分布、成因类型等方面逐渐显示出复杂性和多样性特征.为了进一步探究该地区铅锌多金属矿床的差异性及其内在因素，在前期对白音诺尔、拜仁达坝、维拉斯托、浩布高和边家大院等铅锌多金属矿床研究基础上，结合区内前人对中型以上铅锌多金属矿床的资料和成果，重点讨论了区域上中生代与岩浆作用有关的铅锌多金属矿床成矿背景、共性特征和成矿时空规律，获得了以下主要认识：(1)大部分矿床空间上大致以北、中、南近平行的三条NE向矿带展布，其中一南带矿床尤为密集；(2)时间上可分为中-晚三叠世与晚侏罗-早白垩世两期，且后者的矿床数量占大多数，多期次成矿的现象较为普遍；(3)成因类型上，北矿带主要为浅成低温热液型矿床，中、南成矿带则以矽卡岩型和岩浆热液脉型最为重要；(4)在晚侏罗-早白垩世区域范围内的拉伸环境下，大规模的中酸性岩浆侵入活动是大兴安岭地区最重要岩浆-热事件，形成了多种类型的铅锌多金属矿床，其中的高分异花岗岩与南带富锡铅锌多金属成矿的关系密切；(5)F、Mn元素相关的蚀变与矿化具有较为强烈的空间联系；(6)S同位素显示北带矿床的S来源主要为相关的火山-次火山岩，中带矿床S主要来自成矿岩浆，而南带矿床除岩浆外，围岩地层对S也有一定贡献；(7)Pb同位素数据显示其主要为造山带混合铅来源，与晚侏罗-早白垩世时期大兴安岭地区后造山伸展构造环境有关；(8)H-O同位素数据表明区域矿床的成矿流体来源较为相似，浅成低温热液型矿床流体中大气降水比重较大，而矽卡岩型和岩浆热液脉型矿床则主要为岩浆水，大气降水则在成矿晚期加入.Abstract: As breakthrough achieved in recent exploration,lead-zinc polymetallic deposits in the Great Xing'an Range have shown complexity and differences in aspects of mineralized elements,temporal-spatial distribution,genesis and so on. For a further inspection of the variation and its internal causes,data from medium-large sized deposits are compiled and compared in this study. Main conclusions are summarized: (1) these deposits formed three parallel NE trending belts with a higher intensity in the southern belt; (2) two major phases of mineralization are recognized as in the Middle-Late Triassic (less important) and the predominant Late Jurassic-Early Cretaceous,superimposed mineralization is also notable; (3) epithermal deposit is representative in the northern belt,while skarn- and magmatic hydrothermal vein-types are more common in the middle and the southern belts; (4) under the Late Jurassic-Early Cretaceous extensional environment,enormous acidic-intermediate magma emplacement affected the whole Great Xing'an Range,leading to the formation of various lead-zinc polymetallic deposits,among which tin-rich ones in the southern belt exhibit genetic links to highly differentiated magma; (5) strong spatial association between the fluorine-,manganese-related alteration and mineralization is noticed; (6) deposits in the northern,middle and southern belts have their sulfur sourced from genetically related volcanic-subvolcanic rocks,ore-related magma and a combination of magma and country rocks; (7) Pb isotope data indicate that most deposits have a mixed lead source from orogeny,probably due to similar regional post-orogenic background in the Late Jurassic-Early Cretaceous; (8) as suggested by H-O isotopic data,meteoric water contributes more for fluid source in epithermal deposits,despite a more crucial role of magmatic water in skarn- and magmatic hydrothermal vein-type deposits.
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Key words:
- Great Xing'an Range /
- lead-zinc deposit /
- deposit geology /
- metallogeny belt /
- genetic model
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图 1 大兴安岭地区构造单元划分(a)；大兴安岭地区铅锌矿分布(b)
据Wu et al.(2011)；孟凡超等(2014)；Liu et al.(2017)有修改.F1.德尔布干断裂；F2.新林-喜桂图断裂；F3.贺根山-黑河断裂；F4.嫩江断裂；F5.西拉木伦断裂
Fig. 1. Sketch map of tectonic division in the Great Xing'an Range (GXR) (a), distribution of lead-zinc polymetallic deposits in GXR (b)
图 2 大兴安岭地区铅锌矿床燕山期成岩成矿年龄分布
数据来源见表 1
Fig. 2. Temporal distribution of lead-zinc polymetallic deposits with Yanshanian age in GXR
图 3 大兴安岭地区铅锌矿床成矿岩体的A/NK-A/CNK图解(a)、K2O-SiO2图解(b)和Na2O+K2O-SiO2图解(c)
全岩数据来源:甲乌拉(杨梅等, 2017)、额仁陶勒盖(许立权等, 2014)、八岔沟(刘承先, 2019)、二道河(衮民汕, 2016；本文未发表数据)、朝不楞(Wu et al., 2017)、查干敖包(张万益等, 2012)、吉林宝力格(张万益, 2008)、浩布高(王祥东, 2017)、双尖子山(王祥东, 2017)、白音诺尔(江思宏等, 2011)、维拉斯托(Wang et al., 2017；刘怀征, 2017)、白音查干(刘新等, 2017b；姚磊等, 2017)、大井(Mei et al., 2014)、边家大院(王喜龙, 2014；Ruan et al., 2015)、黄岗(Mei et al., 2015).a.据Maniar and Piccoli(1989)；b.实线据Peccerillo and Taylor(1976), 虚线据Middlemost(1985)；c.据Middlemost(1994)；IR线据Irvine and Baragar(1971)；Ir-Irvine分界线, 上方为碱性, 下方为亚碱性.1.橄榄辉长岩；2a.碱性辉长岩；2b.亚碱性辉长岩；3.辉长闪长岩；4.闪长岩；5.花岗闪长岩；6.花岗岩；7.硅英岩；8.二长辉长岩；9.二长闪长岩；10.二长岩；11.石英二长岩；12.正长岩；13.副长石辉长岩；14.副长石二长闪长岩；15.副长石二长正长岩；16.副长正长岩；17.副长深成岩；18.霓方钠岩/磷霞岩/粗白榴岩
Fig. 3. Plots of A/NK-A/CNK(a), K2O-SiO2(b) and Na2O+K2O-SiO2(c)
图 4 大兴安岭地区铅锌矿床成矿岩体的微量元素蛛网图(a, b, c)与稀土元素配分图(d, e, f)
球粒陨石数据与原始地幔数据来自Sun and McDonough(1989)
Fig. 4. Plots of trace element spider (a, b, c) and REE pattern (d, e, f) diagrams
图 5 大兴安岭地区铅锌矿床成矿岩体的(Na2O+K2O)/CaO-Zr+Nb+Ce+Y图解(a)和Na2O-K2O图解(b)
a.底图据Whalen et al.(1987)；b.底图据Collins et al.(1982)
Fig. 5. Plots of (Na2O+K2O)/CaO-Zr+Nb+Ce+Y (a) and Na2O-K2O(b)
图 6 大兴安岭地区铅锌矿床成矿岩体的Rb/Sr-SiO2图解(a)和SiO2-Al2O3/(CaO+Na2O+K2O)图解(b)
a.底图据Blevin and Chappell(1995)；b.修改自Feiss(1978)
Fig. 6. Plots of Rb/Sr-SiO2 (a) and SiO2-Al2O3/(CaO+Na2O+K2O) (b)
图 7 大兴安岭地区铅锌矿床成矿岩体的δEu-Rb/Sr图解(a)、(Al2O3+CaO)/(FeOt+Na2O+K2O)-100(MgO+FeOt+TiO2)/SiO2图解(b)和K/Rb-SiO2图解(c)
底图据Blevin(2004)
Fig. 7. Plots of δEu-Rb/Sr (a), (Al2O3+CaO)/(FeOt+Na2O+K2O)-100(MgO+FeOt+TiO2)/SiO2 (b) and K/Rb-SiO2 (c)
图 8 大兴安岭地区铅锌矿床成矿岩体的εHf(t)-t图解(a)和εNd(t)-(87Sr/86Sr)t图解(b)
全岩同位素数据来源:甲乌拉(杨梅, 2017)、八岔沟(刘承先, 2019)、二道河(本文未发表数据)、查干敖包(张万益, 2008)、吉林宝力格(张万益, 2008)、浩布高(王祥东, 2017)、双尖子山(王祥东, 2017)、白音诺尔(江思宏等, 2011)、黄岗(Mei et al., 2015)；a.底图据Vervoort et al., 1996；b.底图据Wu et al., 2002
Fig. 8. Plots of εHf(t)-t (a) and εNd(t)-(87Sr/86Sr)t (b)
图 9 大兴安岭地区铅锌矿床黄铁矿、闪锌矿和方铅矿硫同位素特征
硫同位素数据来源:得耳布尔(吕莹玉, 2017)、东珺(温亦品, 2015)、甲乌拉(翟德高等, 2013；Li et al., 2015；牛斯达, 2017)、额仁陶勒盖(田京, 2015)、八岔沟(刘承先, 2019)、二道河(衮民汕, 2016)、朝不楞(聂凤军等, 2007b；陈鹏飞, 2018)、查干敖包(张万益, 2008)、吉林宝力格(张万益, 2008；杜昊, 2018)、阿尔哈达(柯亮亮, 2017；李顺达, 2019)、扎木钦(何鹏等, 2018)、昌图希力(Zhang et al., 2020；何鹏等, 2019)、白音诺尔(曾庆栋等, 2007)、浩布高(李剑锋等, 2015；王祥东, 2017)、黄岗(周振华, 2011)、花敖包特(陈永清等, 2014；张雪冰, 2017)、孟恩陶勒盖(朱笑青等, 2004)、布黑金(付丽娟, 2016)、白音查干(聂凤军等, 2007a)、大井(冯建忠等, 1994；储雪蕾等, 2002)、双尖子山(吴冠斌等, 2014；王祥东, 2017)、拜仁达坝(欧阳荷根, 2013)、维拉斯托(欧阳荷根, 2013)、边家大院(阮班晓等, 2013；Song et al., 2019；Zhai et al., 2019)
Fig. 9. 34SCDT value comparison of pyrite, sphalerite and galena from different deposits in the GXR
图 10 207Pb/204Pb-206Pb/204Pb增长曲线(a)；208Pb/204Pb-206Pb/204Pb增长曲线(b)；207Pb/204Pb-206Pb/204Pb构造环境判别图解(c)；208Pb/204Pb-206Pb/204Pb构造环境判别图解(d)
Pb同位素数据来源:北带:二道河子(李进文等, 2011)、得耳布尔(关键东等, 2015)、东珺(温亦品, 2015)、甲乌拉(翟德高等, 2013；Li et al., 2015)、额仁陶勒盖(田京, 2015), 中带:二道河(衮民汕, 2016)、阿尔哈达(张万益等, 2007)、查干敖包(张万益, 2008)、吉林宝力格(王治华等, 2014；杜昊, 2018)、朝不楞(聂凤军等, 2007b), 南带:扎木钦(何鹏等, 2018)、浩布高(李剑锋等, 2015；王祥东, 2017)、双尖子山(王祥东, 2017)、白音诺尔(江思宏等, 2011)、大井(储雪蕾等, 2002)、黄岗(翟德高等, 2012)、拜仁达坝(欧阳荷根, 2013)、维拉斯托(欧阳荷根, 2013)、边家大院(阮班晓等, 2013).底图据Zartman and Doe(1981)；朱炳泉(1998)
Fig. 10. 207Pb/204Pb-206Pb/204Pb growth curve (a), 208Pb/204Pb-206Pb/204Pb growth curve (b), 207Pb/204Pb-206Pb/204Pb tectonic discriminaton diagram (c), 208Pb/204Pb-206Pb/204Pb tectonic discriminaton diagram (d)
图 11 大兴安岭地区铅锌矿床H-O同位素特征(底图据Sheppard, 1977)
H-O同位素数据来源:甲乌拉(翟德高等, 2013；Li et al., 2015)、额仁陶勒盖(田京, 2015；赵岩, 2017)、得耳布尔(赵岩等, 2018)、二道河(衮民汕, 2016)、阿尔哈达(柯亮亮, 2017；李顺达, 2019)、吉林宝力格(杜昊, 2018)、黄岗梁(周振华等, 2011；梅微等, 2015)、白音诺尔(于琪等, 2015)、浩布高(李剑锋等, 2015)、孟恩陶勒盖(朱笑青等, 2004)、花敖包特(周顶, 2014；张雪冰, 2017)、布金黑(付丽娟, 2016；张雪冰, 2017)、边家大院(阮班晓、吕新彪, 2014；李昊星, 2019)、拜仁达坝(欧阳荷根, 2013；梅微等, 2015)、维拉斯托(欧阳荷根, 2013；梅微等, 2015)、大井(梅微, 2014)
Fig. 11. δDSMOW versus δ18Owater diagram of different deposits in the GXR(modified after Sheppard, 1977)
图 12 大兴安岭地区铅锌矿床铅锌主成矿阶段成矿温度
Fig. 12. Mineralization temperature comparsion of major lead-zinc stage in different deposits
图 13 大兴安岭地区铅锌矿床成矿模式
Fig. 13. Metallogenic model of lead-zinc polymetallic deposits in the Great Xing'an range
表 1 大兴安岭地区铅锌多金属矿床特征
Table 1. Characteristics of lead-zinc polymetallic deposits in the GXR
矿床名称 成因类型 矿化元素 规模 赋矿地层及时代 控矿构造 围岩蚀变 重要金属矿物 成矿岩体与锆石年龄 成矿年代与定年方法 得耳布尔 浅成低温热液型 Pb-Zn-Ag 大型 中侏罗统塔木兰沟组(J2t)粗安岩、安山岩 NW向断裂 内带泥化, 中带硅化、绢云母化, 外带青磐岩化 方铅矿、闪锌矿、黄铜矿、深红银矿、脆银矿、黄铁矿、铅矾、白铅矿、菱锌矿 正长斑岩(燕山晚期) 闪锌矿Rb-Sr等时线141.6± 1.9 Ma (赵岩等, 2017) 比利亚谷 浅成低温热液型 Pb-Zn-Ag 大型 中侏罗统塔木兰沟组(J2t)英安岩、角砾凝灰岩、安山质火山碎屑岩等 NW向张性断裂 线型硅化、黄铁矿化、重晶石化、绢云母化、绿泥石化, 面型青磐岩化 方铅矿、闪锌矿、黄铁矿、黄铜矿 未发现 晚侏罗世 二道河子 低硫化浅成低温热液型 Pb-Zn-Ag 大型 中侏罗统塔木兰沟组(J2t)凝灰岩、岩屑晶屑凝灰岩 NW向张性断裂 硅化、绢云母化、黄铁矿化、碳酸盐化、绿泥石化 方铅矿、闪锌矿、黄铁矿、黄铜矿、毒砂、辉银矿、深红银矿、脆银矿、银黝铜矿 安山玢岩(133.9± 0.9 Ma) (Xu et al., 2020) 闪锌矿Rb-Sr等时线130.5± 3.6 Ma (Xu et al., 2020) 东珺 浅成低温热液型 Pb-Zn-Ag 中型 中侏罗统塔木兰沟组(J2t)玄武安山岩、粗安岩、凝灰岩 NW向张性断裂 硅化、绢云母化、碳酸盐化、高岭土化、绿泥石化、少量阳起石化 方铅矿、闪锌矿、黄铜矿、黄铁矿、磁黄铁矿、毒砂、磁铁矿 未发现 闪锌矿Rb-Sr等时线130.2± 4.4 Ma (杨郧城等, 2015) 甲乌拉 低硫化浅成低温热液型 Ag-Pb-Zn-Cu 大型 中侏罗统塔木兰沟组(J2t)安山岩、安山质火山碎屑岩 NNW、NWW向断裂、放射状断裂系统、层间构造带 硅化、绿泥石化、碳酸盐化、水云母和伊利石化、萤石化 方铅矿、闪锌矿、黄铜矿、黄铁矿、磁黄铁矿、毒砂、磁铁矿 富碱花岗斑岩(146.4±1.6 Ma；杨梅等, 2017) 硫化物Rb-Sr等时线142.7± 1.3 Ma(李铁刚等, 2014)；热液锆石U-Pb 143.1±3.9 Ma(杨梅等, 2017) 查干布拉根 低硫化浅成低温热液型 Ag-Pb-Zn 大型 中侏罗统万宝组(J2w)砂岩、砾岩, 塔木兰沟组(J2t)玄武岩、安山岩 硅化、碳酸盐化、伊利石化、水云母化、绿泥石化、高岭土化、绢云母化、萤石化 方铅矿、闪锌矿、黄铁矿、黄铜矿、磁黄铁矿、毒砂、硫锑铜银矿、银黝铜矿、深红银矿、硫银锡矿、辉银矿、金银矿、银金矿、自然金 未发现 白云母Ar-Ar坪年龄137.7± 0.94 Ma (Li et al., 2016) 额仁陶勒盖 低硫化浅成低温热液型 Ag-Pb-Zn-Mn 大型 中侏罗统塔木兰沟组(J2t)玄武岩、安山岩、火山碎屑岩 NE向扭性断裂、NW向张扭性断裂 中心向外围依次为硅化、绢英岩化、泥化、青磐岩化、碳酸盐化 硬锰矿、自然银、黄铁矿、方铅矿、闪锌矿、黄铜矿 石英二长斑岩脉(138.6±2.3 Ma；许立权等, 2014) 早白垩世 八岔沟 矽卡岩型 Pb-Zn-Ag 大型 上侏罗统满克头鄂博组(J3mk)流纹质晶屑凝灰岩 NE和NW向断裂及两者交汇处 矽卡岩化、碳酸盐化、云英岩化、硅化、绢云母化、绿泥石化、高岭土化 闪锌矿、方铅矿、磁铁矿、黄铁矿、黄铜矿 黑云母二长花岗岩(141.5± 1.1 Ma；刘承先, 2019) 早白垩世 二道河 矽卡岩型 Pb-Zn-Ag 大型 中上奥陶统裸河组(O2-3l)灰岩、变质粉砂岩；次为中侏罗统塔木兰沟组(J2t)安山岩 NE向断裂 矽卡岩化、绿帘石化、碳酸盐化、绿泥石化、绢云母化、硅化、钾长石化、钠长石化、萤石化 闪锌矿、方铅矿、黄铜矿、黄铁矿、磁黄铁矿、磁铁矿、赤铁矿、硫锰矿 二长闪长岩(227±2 Ma；Yang et al., 2020)、闪长玢岩脉(145.0±1.6 Ma；杨发亭, 2016)、花岗斑岩脉(134±1 Ma；衮民汕, 2016) 热液榍石U-Pb 234.0±5.9 Ma、144.4± 3.9 Ma(本文未发表数据)；闪锌矿Rb-Sr等时线131±2 Ma(衮民汕, 2016) 朝不楞 矽卡岩型 Fe-Bi-Ag-Sn-(Cu-Pb-Zn-W-Mo) 中型(小型) 中泥盆统塔尔巴格特组(D2t)板岩、粉砂岩、凝灰岩、碳酸盐岩和细砂岩 NE向断裂破碎带 矽卡岩化、钙硅质角岩化、绿帘石化、碳酸盐化、萤石化、硅化、钾化、绿泥石化、泥化 磁铁矿、赤铁矿、白钨矿、毒砂、斜方砷铁矿、白铁矿、辉钼矿、黄铜矿、磁黄铁矿、闪锌矿、方铅矿、辉铋矿、斜方辉铅铋矿、自然铋 朝不楞复式岩体(130~145 Ma, 137.07± 0.57 Ma；Wu et al., 2017) 辉钼矿Re-Os等时线外接触带140.7±1.8 Ma(聂凤军等, 2007b), 内接触带131.2± 4.1 Ma、135.0± 2.1 Ma(Wu et al., 2017) 阿尔哈达 岩浆热液脉型 Pb-Zn-Ag 大型 上泥盆统安格尔音乌拉组(D3a)炭质板岩、细砂岩和凝灰岩 NW向断裂 高岭土化、绢云母化、白云母化、绿泥石化、绿帘石化、硅化、滑石化、碳酸盐化、萤石化 方铅矿、闪锌矿、黄铁矿、毒砂、磁黄铁矿、黄铜矿、黝锡矿 隐伏黑云母花岗岩(156.27±0.49 Ma；李顺达, 2019) 白云母Ar-Ar坪年龄156.27± 0.49 Ma (谢玉玲等, 2015) 查干敖包-曼特敖包 矽卡岩型 Fe-Zn 中型 中奥陶统多宝山组(O2d)大理岩-凝灰质板岩 NE向断裂及其次级断裂和构造破碎带 矽卡岩化、角岩化、硅化、高岭土化、绿泥石化、绿帘石化、碳酸盐化 磁铁矿、闪锌矿、赤铁矿、磁黄铁矿、黄铁矿、斑铜矿、毒砂、自然铋、辉铋铅矿、辉钼矿、方铅矿、白钨矿 碱性石英闪长岩(237± 6 Ma；张万益等, 2008) 中晚三叠世 吉林宝力格 岩浆热液脉型 Ag-(Au-Pb-Zn) 中型 上泥盆统安格尔音乌拉组(D3a)粉砂凝灰质泥岩夹砂岩和凝灰砂质板岩 NW向张扭性断裂 角岩化、高岭土化、硅化、绢云母化、绿泥石化、碳酸盐化 毒砂、黄铁矿、白铁矿、黄铜矿、方铅矿、闪锌矿 斑状二长花岗岩(314±8.8 Ma；张万益, 2008) 晚石炭世 扎木钦 浅成低温热液型 Pb-Zn-Ag 大型 下白垩统白音高老组(K1b)英安质角砾凝灰岩、晶屑凝灰岩 NE向层间断裂、NW向张扭性断裂及两者交汇处 高岭土化、绢云母化、白云母化、绿泥石化、绿帘石化、硅化、黄铁矿化、碳酸盐化、萤石化 方铅矿、闪锌矿、黄铁矿、深红银矿、辉银矿、脆银矿、毒砂、针碲金银矿、自然银、银黝铜矿 白音高老组火山岩(早白垩世？) 早白垩世 花敖包特 岩浆热液脉型 Pb-Zn-Ag 大型 下二叠统寿山沟组(P1s)砂岩、粉砂岩、炭质板岩、细砂岩、粉砂质泥岩 NW、NE、NS向断裂及其交汇处 硅化、绢云母化、黄铁矿化、高岭土化、碳酸盐化、绿泥石化 方铅矿、闪锌矿、黄铁矿、磁黄铁矿、毒砂、深红银矿、辉银矿、银黝铜矿、黄铜矿、辉锑矿 流纹斑岩(136±3 Ma；张雪冰, 2017) 早白垩世 布金黑 岩浆热液脉型 Pb-Zn 中型 下二叠统寿山沟组(P1s)变质砂岩、泥质板岩 EW向断裂 硅化、碳酸盐化、绢云母化、绿泥石化、绿帘石化、高岭土化、萤石化 黄铁矿、毒砂、磁黄铁矿、闪锌矿、方铅矿、锡石、辉银矿、斑铜矿 流纹斑岩(122.9± 2.4 Ma；张雪冰, 2017) 早白垩世 昌图希力 中-低硫化浅成低温热液型 Ag-Pb-Zn-Mn 大型 下白垩统白音高老组(K1b)英安岩、流纹岩、流纹质火山碎屑岩 NW向破碎蚀变带 硅化、绿泥石化、绢云母化、泥化、碳酸盐化 菱锰矿、硬锰矿、锰钾矿、锰铅矿、方铅矿、闪锌矿、银黝铜矿、自然银、深红银矿、黄铁矿、毒砂、黄铜矿 白音高老组火山岩(146~160 Ma；Zhang et al., 2020) 晚侏罗世-早白垩世 孟恩陶勒盖 岩浆热液脉型 Ag-Pb-Zn-(Cu-Au-Sn) 大型 无 EW向脆性断裂 硅化、白云母化、绢云母化、绿泥石化、碳酸盐化、锰菱铁矿化 方铅矿、闪锌矿、黄铜矿、黄铁矿、磁黄铁矿、毒砂、锡石、黝锡矿 隐伏花岗岩？ 白云母Ar-Ar坪年龄179.0± 1.5 Ma (张炯飞等, 2003) 浩布高 矽卡岩型 Cu-Pb-Zn-Fe-Sn 大型 下二叠统大石寨组(P1d)粉砂质、泥质板岩夹大理岩、变质砂岩 NE向断裂 矽卡岩化、绢云母化、绿泥石化、钾长石化、云英岩化、青磐岩化 闪锌矿、方铅矿、黄铜矿、磁铁矿、磁黄铁矿、锡石、黄铁矿、赤铁矿 黑云母花岗岩(139 Ma；Wang et al., 2018) 辉钼矿Re-Os等时线137.5± 2.7 Ma (Wang et al., 2018) 双尖子山 岩浆热液脉型 Ag-Pb-Zn 超大型 下二叠统大石寨组(P1d)泥质炭质板岩夹蚀变凝灰岩和蚀变安山岩 NW、NE向断裂 绿泥石化、硅化、碳酸盐化、黄铁矿化 闪锌矿、方铅矿、黄铁矿、毒砂、黄铜矿、硫银锡矿、深红银矿、银黝铜矿、硫锑铜银矿 斑状花岗闪长岩(130± 6 Ma；Liu et al., 2016), 斑状花岗岩(159.3± 2.3 Ma；欧阳荷根等, 2016) 闪锌矿Rb-Sr等时线132.7± 3.9 Ma(吴冠斌等, 2013)；黄铁矿Re-Os等时线165.0± 7.1 Ma (Liu et al., 2016) 白音诺尔 矽卡岩型 Pb-Zn 大型 下二叠统哲斯组(P1z)结晶灰岩、大理岩 NE、EW向断裂及NE向复背斜 矽卡岩化、绿泥石化、绿帘石化、碳酸盐化、硅化、高岭土化 方铅矿、闪锌矿、黄铁矿、黄铜矿、磁黄铁矿、锡石、毒砂、斑铜矿 花岗闪长岩(244.5± 0.9 Ma), 凝灰熔岩(172.9±2.7 Ma)(Jiang et al., 2017) 闪锌矿Rb-Sr等时线167.6± 4.9 Ma (王祥东等, 2019) 拜仁达坝 岩浆热液脉型 Ag-Pb-Zn 大型 下古生界“锡林郭勒杂岩”黑云斜长片麻岩 近EW向压扭性断裂 硅化、绢云母化、萤石化、碳酸盐化、高岭土化 闪锌矿、黄铜矿、方铅矿、磁黄铁矿、毒砂、黄铁矿、辉锑矿、银黝铜矿、硫锑铅矿 未发现 白云母Ar-Ar坪年龄135±3 Ma (常勇和赖勇, 2010) 维拉斯托 岩浆热液脉型 Sn-Pb-Zn-Sn-Cu-Li-Rb 大型 下古生界“锡林郭勒杂岩”黑云斜长片麻岩 近EW向压扭性断裂 绿泥石化、硅化、绢云母化、碳酸盐化、云英岩化、绿帘石化、叶腊石化、高岭土化 锡石、闪锌矿、黄铜矿、黄铁矿、黑钨矿、方铅矿、辉钼矿、黝锡矿、斜方砷铁矿、黝铜矿、磁铁矿、针硫锑铅矿 石英斑岩(135~139 Ma；翟德高等, 2016；祝新友等, 2016) 云英岩锡石U-Pb 138±6、135±6 Ma(Wang et al., 2017)、石英脉锡石136.0±6.1 Ma(刘瑞麟等, 2018) 白音查干 岩浆热液脉型 Sn-Cu-Pb-Zn-Ag-(Sb) 大型 下二叠统大石寨组(P1d)凝灰质粉砂岩 NE、NEE向断裂 电气石化、云英岩化、萤石化、硅化、绢云母化、绿泥石化、碳酸盐化、高岭土化 锡石、闪锌矿、黄铁矿、黄铜矿、方铅矿、辉锑矿、毒砂、黝铜矿、银黝铜矿、脆硫锑铅矿 石英斑岩(140.0~144.3 Ma；姚磊等, 2017；刘新等, 2017b) 早白垩世 大井 岩浆热液脉型 Sn-Ag-Pb-Zn-Cu 大型 上二叠统林西组(P3l)黑色板岩、砂岩夹泥灰岩 NW、NWW向断裂 硅化、绿泥石化、绢云母化、萤石化、碳酸盐化 黄铜矿、锡石、闪锌矿、方铅矿、黄铁矿、毒砂、磁黄铁矿、银矿物 次火山岩脉(162.0~253.8 Ma；Mei et al., 2014；刘铭涛等, 2019) 锡石U-Pb 144±16 Ma (廖震等, 2014) 边家大院 岩浆热液脉型 Pb-Zn-Ag-Sn-Mo 中型 下二叠统哲斯组(P1z)硅质粉砂岩 NW向断裂 绿泥石化、硅化、绢云母化、黄铁矿化、钾化、碳酸盐化 方铅矿、闪锌矿、磁黄铁矿、黄铁矿、黄铜矿、辉银矿、银黝铜矿、深红银矿、硫砷铜银矿 石英斑岩(140.8± 0.9 Ma、140.2± 0.6 Ma；Ruan et al., 2015；Zhai et al., 2017) 辉钼矿Re-Os 140.0±1.7 Ma；绢云母Ar-Ar坪年龄138.7±1.0 Ma(Zhai et al., 2017) 黄岗 矽卡岩型 Fe-Sn-(Pb-Zn) 大型 下二叠统哲斯组(P1z)安山岩、P1h大理岩 NE向断裂 矽卡岩化、萤石化、碳酸盐化、硅化 磁铁矿、锡石、白钨矿、闪锌矿、黄铜矿、方铅矿、毒砂、辉钼矿、辉铋矿、磁黄铁矿、黄铁矿 钾长花岗岩(139~145 Ma；Mei et al., 2015；Zhai et al., 2014) 辉钼矿模式年龄141.2±4.3 Ma(团块状矽卡岩)、264.8± 3.9 Ma(似层状矽卡岩)(要梅娟等, 2016) 
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表 2 大兴安岭地区铅锌多金属成矿带特征对比
Table 2. Characteristic comparison of lead-zinc polymetallic belts in the Great Xing'an Range
北带 中带 南带 主要成因类型 浅成低温热液型 矽卡岩型、岩浆热液脉型 主矿化元素 Pb-Zn-Ag Pb-Zn-Ag-Sn(-Fe-Cu) 主要赋矿地层 中侏罗世火山(碎屑)岩 奥陶-泥盆系碎屑沉积岩 二叠系碎屑沉积岩 主要成矿岩体 火山-次火山岩 中酸性侵入岩 高分异岩浆 成矿物质S来源 火山-次火山岩 中酸性侵入岩 成矿岩浆及围岩地层 主要成矿流体来源 大气降水 岩浆水混合大气降水
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