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南秦岭柞水−山阳矿集区金盆梁金矿床载金硫化物矿物学特征及成矿指示

葛战林, 顾雪祥, 章永梅, 郑艳荣, 刘明, 郝迪, 王元伟

葛战林, 顾雪祥, 章永梅, 等. 南秦岭柞水−山阳矿集区金盆梁金矿床载金硫化物矿物学特征及成矿指示[J]. 西北地质, 2023, 56(5): 278-293. DOI: 10.12401/j.nwg.2023118
引用本文: 葛战林, 顾雪祥, 章永梅, 等. 南秦岭柞水−山阳矿集区金盆梁金矿床载金硫化物矿物学特征及成矿指示[J]. 西北地质, 2023, 56(5): 278-293. DOI: 10.12401/j.nwg.2023118
GE Zhanlin, GU Xuexiang, ZHANG Yongmei, et al. Mineralogical Characteristics and Metallogenic Indication of Gold−Bearing Sulfides in the Jinpenliang Gold Deposit, Zhashui−Shanyang Ore Cluster Area, South Qinling[J]. Northwestern Geology, 2023, 56(5): 278-293. DOI: 10.12401/j.nwg.2023118
Citation: GE Zhanlin, GU Xuexiang, ZHANG Yongmei, et al. Mineralogical Characteristics and Metallogenic Indication of Gold−Bearing Sulfides in the Jinpenliang Gold Deposit, Zhashui−Shanyang Ore Cluster Area, South Qinling[J]. Northwestern Geology, 2023, 56(5): 278-293. DOI: 10.12401/j.nwg.2023118

南秦岭柞水−山阳矿集区金盆梁金矿床载金硫化物矿物学特征及成矿指示

基金项目: 国家自然科学基金重点项目“新疆西天山北缘晚古生代斑岩−矽卡岩型铜钼铁多金属成矿与岩浆−热液作用过程”(42130804),中国地质调查局项目“东秦岭高岭沟−五里川一带锑金矿产调查评价”(ZD20220306),陕西省自然科学基础研究计划资助项目(2023-JC-QN-0284)联合资助。
详细信息
    作者简介:

    葛战林(1992−),男,博士研究生,工程师,主要从事矿床学及矿床地球化学研究。E−mail:gezhanlin@163.com

    通讯作者:

    顾雪祥(1963−),男,教授,博士生导师,主要从事矿床学及矿床地球化学研究。E−mail:xuexaing_gu@cugb.edu.cn

  • 中图分类号: P575.1;P618.51

Mineralogical Characteristics and Metallogenic Indication of Gold−Bearing Sulfides in the Jinpenliang Gold Deposit, Zhashui−Shanyang Ore Cluster Area, South Qinling

  • 摘要:

    金盆梁金矿床位于南秦岭柞水−山阳金多金属矿集区北部,矿体呈近东西向赋存于上泥盆统桐峪寺组的沉积建造中,受左行韧性断层控制。关于矿石矿物学与金成矿过程尚缺乏系统的认识。基于岩矿相学鉴定、背散射电子图像(BSE)、能谱(EDS)及电子探针分析(EPMA)等方法,查明矿石组构与载金硫化物毒砂、黄铁矿、辉锑矿及白铁矿的矿物学特征,探讨金的赋存状态与成矿物理化学条件,初步厘定矿床成因类型。结果显示,热液成矿期的金矿化以微细浸染型为主,可划分为黄铁矿−毒砂−硅化(Ⅰ)、石英−辉锑矿−白铁矿±锑氧化物(Ⅱ)及方解石−石英(Ⅲ)3个阶段。不同载金硫化物的“不可见金”赋存状态差异显著,由毒砂的晶格金Au+,到早世代黄铁矿(Py-1)的晶格金Au+−纳米金Au0,至晚世代黄铁矿(Py-2)和白铁矿的纳米金Au0。金属矿物组合由毒砂−黄铁矿至辉锑矿−白铁矿,成矿流体由较高温的相对自然金不饱和状态,逐渐演化为相对低温的自然金饱和状态。金盆梁金矿床形成于较高硫逸度的中高温、中浅成环境,属于卡林型金矿床。

    Abstract:

    The Jinpenliang gold deposit is located in the northern part of the Zhashui−Shanyang ore cluster area, South Qinling. The E−W trending main orebodies, occurring in sedimentary rocks of the Upper Devonian Tongyusi Formation, are strictly controlled by the left−lateral ductile faults. To date, there is still insufficient understanding of the ore mineralogy and gold mineralization processes. In this paper, we obtain data from a variety of experimental methods, such as petrographic identification, Back−Scattered Electron imaging (BSE), Energy Dispersive Spectrometry (EDS), and Electron Probe Micro−Analysis (EPMA), to determine the mineralogical characteristics of gold−bearing sulfides (arsenopyrite, pyrite, stibnite, and marcasite), and discuss the chemical states of Au and physicochemical conditions for gold mineralization. The results show that the micro−disseminated gold mineralization in hydrothermal period can be divided into three stages: pyrite−arsenopyrite−silicification stage (Ⅰ), quartz−stibnite−marcasite±antimony oxides stage (Ⅱ), and calcite−quartz stage (Ⅲ). The occurrence states of “invisible gold” vary greatly among different gold−bearing sulfides, from Au+ in arsenopyrite to Au+ and Au0 in early generation pyrite (Py-1), then to Au0 in late generation pyrite (Py-2) and marcasite. The metal mineral assemblage changes from arsenopyrite−pyrite to stibnite−marcasite, while the ore−forming fluid gradually evolves from relatively high−temperature solutions unsaturated with respect to native gold to low−temperature solutions saturated with respect to native gold. The Jinpenliang gold deposit is a Carlin−type gold deposit, which was formed in a medium−high temperature and shallow−moderate depth with logf(S2) ranging from −8.5 to −4.5.

  • 矿石组构与金的赋存状态研究,对于正确理解金的富集机制、矿床成因及优化矿石选冶工艺等具有十分重要的意义(胡文宣等,2001华曙光等,2012)。典型卡林型金矿床的金主要以“不可见金(Invisible gold)”形式赋存于含砷黄铁矿和毒砂等Fe−As−S矿物中(Fleet et al.,1997),但仍存在次显微–纳米级自然金Au0、晶格金Au+、Au及Au3+等诸多不同的认识(Arehart et al.,1993Simon et al.,1999a李九玲等,2002Gopon et al.,2019)。(含As)黄铁矿是造山型与类卡林型金矿最重要的载金矿物,金以自然金和Au–Ag–(Te)系列矿物形式为主(Bateman et al.,2004Goldfarb et al.,2017刘家军等,2019)。毒砂和黄铁矿等载Au硫化物的元素含量、特征比值及相关性分析,可有效厘定Au的赋存状态、反演成矿流体性质和约束成矿物理化学条件,对于金成矿过程、成矿机制及矿床成因的研究至为关键(Kretschmar et al.,1976Reich et al.,2005孙宁岳等,2022)。

    陕甘川“金三角”地区是中国重要的卡林–类卡林型金矿集中区,金主要产出于南秦岭泥盆系和三叠系碳酸盐岩–碎屑岩建造中(陈衍景等,2004),包括寨上、阳山及金龙山等代表性超大型和规模不等的金矿床多达50余处(Liu et al.,2015Ma et al.,2020姜寒冰等,2023)。然而,关于南秦岭沉积岩容矿型金矿床尚存在造山型、卡林型及类卡林型等多种成因认识(毛景文,2001Mao et al.,2002陈衍景等,2004)。柞水–山阳金多金属矿集区位于南秦岭晚古生代弧前盆地,已发现夏家店、王家坪和王家沟等多处卡林型金矿床(丁坤等,20212022);金盆梁即位于矿集区北部,是一处具有中型成矿远景的微细浸染型金矿床(李雪松等,2021)。目前,矿区仍以金锑找矿勘查为主(张嘉升等,2014),有关矿石矿物学与Au赋存状态的研究尚无报道,导致成矿过程与矿床成因认识不清。基于矿床地质特征与矿石组构的研究,笔者以不同成矿阶段的硫化物为研究对象,开展岩矿相学显微鉴定、扫描电镜–能谱及电子探针分析,查明金盆梁金矿床载金矿物的组分特征,限定Au的赋存状态与成矿物理化学条件,初步探讨矿床成因类型,以期为区域金锑成矿过程与成矿规律的研究提供一定依据。

    南秦岭柞水–山阳金多金属矿集区属于秦岭造山带陕西段五大矿集区之一,夹持于北部商丹断裂与南部山阳–凤镇断裂之间的南秦岭弧前盆地(王宗起等,2009王瑞廷等,2021),以北西–北西西向断裂最为发育,且控制着主要矿产的分布特点(图1)(朱赖民等,2019)。

    图  1  秦岭造山带构造单元(a)及柞水–山阳矿集区地质图(b)(据Ding et al.,2022修改)
    1. 第四系;2. 石炭系;3. 泥盆系;4. 下古生界;5. 前寒武系;6. 晚侏罗—早白垩世花岗岩;7. 中—晚三叠世花岗岩;8. 新元古代花岗岩;9. 新元古代闪长岩;10. 辉长–辉绿岩;11. 角闪岩;12. 卡林型金矿床;13. 热水沉积改造型银矿床;14. 热水沉积改造型铜矿床;15. 热水沉积改造型铁矿床;16. 岩浆分结型铁矿床;17. 矽卡岩–斑岩型铜矿床;18. 断层;19. 地质界线;20. 地名
    Figure  1.  (a) Tectonic framework of the Qinliong orogen and (b) geological map of the Zhashui–Shanyang ore district cluster

    区域以泥盆系和石炭系分布最为广泛,山阳–凤镇断裂以北主要为中—上泥盆统(桐峪寺组、青石垭组、池沟组及牛耳川组)浅海–半深海相的浅变质沉积碎屑岩、碳酸盐岩及复理石建造,以及下石炭统的海陆交互相含煤岩系,岩性为砂岩、粉砂岩、板岩及灰岩(Ding et al.,2022);南部则以中—上泥盆统和石炭系的浅海陆棚碎屑岩、碳酸盐建造为主(王瑞廷等,2021)。中生代陆内构造–岩浆活动与成矿作用极为强烈,以东江口为代表的印支期花岗岩呈近东西向分布于矿集区北部(230~210 Ma)(葛战林等,2021);燕山期浅成–超浅成的小斑岩体多侵位于北西–北西西向与南北向断层的交汇部位,成岩年龄大多为150~140 Ma(谢桂青等,2012吴发富等,2014朱赖民等,2019Zhang et al.,2021李平等,2023),与晚侏罗世—早白垩世的Au、Cu(Mo)成矿关系密切(刘凯等,2019丁坤,2020)。

    区内矿产资源丰富,以Au、Ag、Cu、Fe为优势矿种,典型矿床有银硐子–大西沟特大型热水沉积改造型银多金属矿(方维萱等,2000)、夏家店大型微细浸染型金矿(高菊生等,2006刘凯等,2019)及小河口中型斑岩型铜矿(熊潇等,2019)等。截至目前,已发现大小金矿床(点)20余处,大多沿山阳–凤镇断裂的南北两侧展布(图1),而王家沟、金盆梁金矿则位于矿集区的最北端。

    金盆梁金矿位于陕西省柞水县瓦房口镇,大地构造位置处于南秦岭北部晚古生代裂陷带(张国伟等,2019),与区域王家沟金矿床同处于Ⅳ-66B-5山阳–柞水华力西—燕山期Fe–Ag–Cu–Pb–Zn–金红石成矿亚带(陕西省地质调查院,2017)。

    矿区主要出露上泥盆统(D3)、上泥盆统桐峪寺组(D3t)及下石炭统二峪河组(C1e)。其中,上泥盆统分布于F13断裂以北,可对比于区域下古生界罗汉寺组,以浅变质的火山–沉积岩系为特征区别于桐峪寺组(张亚峰等,2022),仅个别矿化带赋存于其绿灰色千枚状含凝灰质石英粉砂岩中(图2)。上泥盆统桐峪寺组是最主要的赋矿地层,呈近东西向分布于F18断裂以南,属一套浅海–滨海相沉积碎屑岩建造(闫臻等, 2014)。矿脉几乎全部赋存于第五岩性段(D3t5)与第六岩性段(D3t6)中,岩性包括灰色千枚状粉砂质板岩、钙质板岩、灰褐黄色变质石英粉砂岩及灰绿色变质长石石英细砂岩,夹薄层细晶–粉晶灰岩等。二峪河组呈近东西向带状分布于矿区中部,岩性组合为中薄层灰岩、石英粉砂岩、粉砂质板岩及绢云千枚岩等。

    图  2  金盆梁金矿床地质图(据苏选民等,2012
    1. 下石炭统二峪河组上亚组下段;2. 下石炭统二峪河组下亚组上段;3. 上泥盆统(未分);4. 上泥盆统桐峪寺组第六岩性段;5. 上泥盆统桐峪寺组第五岩性段上亚段;6. 上泥盆统桐峪寺组第五岩性段下亚段;7. 上泥盆统桐峪寺组第四岩性段上亚段;8. 二长花岗岩;9. 闪长玢岩脉;10. 云斜煌斑岩脉;11. 矿体及编号;12. 矿化体;13. 断层及编号;14. 地名
    Figure  2.  Geological map of the Jinpenliang gold deposit

    近东西向曹坪–红岩寺复式向斜与断裂构成了矿区的主要构造格架,后期叠加北西向、北东向走滑断裂。北东向左行走滑断层是本区主要的导矿构造,出露于矿区南部,一般长为313~4154 m,宽为1~5 m,走向为25°~40°,倾向北西,倾角为65°~80°;断面平直光滑,带内主要由糜棱岩、透镜状角砾组成,硅化、绿泥石化强烈。矿区岩浆活动较为强烈,北部见印支期曹坪二长花岗岩侵位于上泥盆统,闪长玢岩脉和云斜煌斑岩脉亦有发育。

    目前,金盆梁金矿床共发现矿脉14条,圈定Ⅰ-1、Ⅱ-1金矿体2个(图2)。Ⅰ-1主矿体呈透镜体状分布于玄檀沟一带,赋存标高为1264~1506 m,地表槽探控制矿体长为593 m,深部坑道控制斜深为242 m。矿体由毒砂–黄铁矿–辉锑矿–硅化粉砂质板岩组成(图3),呈近东西走向,向南陡倾(180°~185°∠80°~85°),厚度为0.80~7.25 m,平均厚为1.76 m;金品位为2.57~12.36 g/t,平均金品位为4.53 g/t,估算推断资源量为783 kg(苏选民等,2012)。因受左行韧性剪切构造控制,矿体与围岩界线较为清晰,近矿围岩蚀变以硅化、绢云母化及毒砂–黄铁矿化为主,远端则碳酸盐化较强。

    图  3  金盆梁金矿床典型矿体与矿石照片
    a. 主矿体赋存于粉砂质板岩的断裂中,石英–辉锑矿细脉切穿毒砂–黄铁矿化蚀变岩;b. 受左行韧性剪切作用,石英–辉锑矿脉呈浅黄色透镜状产出;c. 矿体远端的方解石–石英脉;d. 毒砂–黄铁绢英岩型矿石;e. 石英–辉锑矿脉型矿石;f. 方解石–石英脉手标本;g. 毒砂、黄铁矿呈微细浸染状,见自形毒砂沿边部交代他形粗粒黄铁矿;h. 辉锑矿呈半自形晶,含少量白铁矿;i. 方解石细脉切穿粗粒石英;j-l. Ⅰ~Ⅲ阶段的非金属矿物特征;Py. 黄铁矿;Apy. 毒砂;Stb. 辉锑矿;Mrc. 白铁矿;Q. 石英;Cal. 方解石;Ser. 绢云母
    Figure  3.  Photos of typical orebodies and ores of the Jinpenliang gold deposit

    根据矿化类型、脉体穿切关系及矿物共生组合特征,金盆梁金矿床热液成矿期可划分为3个成矿阶段:黄铁矿–毒砂–硅化阶段(Ⅰ),金属矿物含量约为5%~8%,主要为微细浸染状的黄铁矿和毒砂,偶见辉锑矿,硫化物集合体局部呈宽约为1 mm的细脉(图3d)。黄铁矿呈他形–半自形粒状晶,粒径为0.02~0.60 mm;毒砂以亮白色微带奶油色的针柱状、矛状及菱形自形晶为特征,多沿早世代黄铁矿边部交代或呈放射状集合体,粒径大小为0.01~0.20 mm(图3g)。石英–辉锑矿–白铁矿±锑氧化物阶段(Ⅱ),呈宽3~5 cm的灰白–黄白色细脉切穿毒砂–黄铁矿化蚀变岩(图3a),强烈透镜体化(图3b)。其中,石英呈烟灰色–灰白色,结晶较好;针柱状辉锑矿集合体呈团斑状充填于脉体中,大小为0.50×1.0 cm~1.0×3.0 cm,局部氧化为浅黄色锑华和黄锑矿等(图3e、图3h)。方解石–石英阶段(Ⅲ),呈宽为3~7 cm宽的白色–黄白色陡倾细脉–网脉(图3c),密集发育于矿体远端;主要由方解石和石英组成,含少量绢云母、白云石(图3f、图3i),偶见星点状金属矿物。

    样品均采自金盆梁金矿区LDX01老硐Ⅰ-1主矿体,包括毒砂–黄铁绢英岩型(Ⅰ阶段)、石英–辉锑矿脉型矿石(Ⅱ阶段)及无矿方解石–石英脉(Ⅲ阶段),采样坐标为 E 109°27′27″,N 33°42′25″。优选典型样品开展矿物学鉴定与实验测试。

    岩矿相学鉴定在中国地质调查局西安矿产资源调查中心实验室完成,仪器为德国莱卡DM2500P偏光显微镜。背散射电子图像(BSE)、能谱(EDS)和电子探针分析(EPMA)在西北大学大陆动力学国家重点实验室完成,仪器型号为JEOL JAX-8230,分析精度≤ ± 2%,最低检测限为~0.001%。测试条件:加速电压为15 kV,电子束电流为10 nA,束斑直径为2 μm。标样由美国SPI公司提供:Au(Au)、FeS2(Fe, S)、PbS(Pb)、Bi(Bi)、Ag(Ag)、Cd(Cd)、Sb2Te3(Sb, Te)、Se(Se)、FeAsS(As)、ZnS(Zn)、Cu(Cu)、Ni(Ni)、Co(Co)、Mn(Mn)和TiO2(Ti)。

    矿石类型以毒砂–黄铁绢英岩型为主(图3d),次为石英–辉锑矿脉型(图3e)。毒砂–黄铁矿化蚀变岩主要产于赋矿断裂内部,以发育微细浸染状毒砂、黄铁矿为特征;呈稀疏微细浸染状、细脉浸染状构造,具自形–半自形结构、他形结构、浸蚀结构、包含结构及弱增生环带结构。石英–辉锑矿脉沿毒砂–黄铁绢英岩裂隙充填,矿石以细脉–网脉状、团块状构造为主,多见半自形–他形结构、交代残余结构等(表1)。

    表  1  金盆梁金矿床矿石类型与硫化物特征表
    Table  1.  Ore types and sulfide characteristics of the Jinpenliang gold deposit
    矿石类型金属硫化物特征描述素描图
    毒砂–黄铁绢英岩型 Apy 毒砂(Apy)呈亮白色针柱状、菱形、茅状自形晶,常见晶面裂纹与孔隙;呈独立放射状或沿早世代黄铁矿边部交代形成毒砂–黄铁矿集合体

    Py-1 早世代黄铁矿(Py-1)呈浅黄色–黄白色中粗粒他形晶,孔隙与裂纹发育;内部结构均一,增生环带不明显,边部多被自形–半自形毒砂交代浸蚀
    Py-2 晚世代黄铁矿(Py-2)呈黄白色细粒自形–半自形晶,孔隙与裂纹较少,内部为均质结构;多独立产出,偶见内部包含自形毒砂颗粒
    石英–辉锑矿脉型 Stb 辉锑矿(Stb)反射色为白色–灰白色,多色性极为显著,多呈半自形针柱状、粒状晶,易磨光,常见擦痕。可见白铁矿、黄锑矿(Cvn)等交代辉锑矿
    Mrc 白铁矿(Mrc)呈浅黄白色自形板柱状晶,以似节理状的密集条纹切面为鉴别特征,大多沿辉锑矿边部或内部交代产出,极少数独立赋存于石英中
    下载: 导出CSV 
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    毒砂、黄铁矿、辉锑矿和白铁矿均属于金盆梁金矿的载金硫化物。其中,毒砂(Apy)主要以稀疏浸染状赋存于毒砂–黄铁绢英岩型矿石中,呈亮白色针柱状、菱形、茅状自形晶,大小为10~200 μm,晶面裂纹、孔隙较为发育(图4a),背散射电子图像呈明亮的均质结构(图4b);呈独立放射状和毒砂–黄铁矿集合体形式产出(图4c)。

    图  4  金盆梁金矿石硫化物显微特征图
    a~d. 毒砂沿早世代黄铁矿边部或内部交代,构成毒砂–黄铁矿聚合体,见晚世代黄铁矿包含自形细粒毒砂;e~g. 辉锑矿呈自形–半自形粒状,白铁矿和锑氧化物交代辉锑矿;h~i. 黄锑矿和白铁矿的能谱图;Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Stb. 辉锑矿;Mrc. 白铁矿;Cvn. 黄锑矿;Q. 石英
    Figure  4.  Microscopic characteristics of sulfides in ores of the Jinpenliang gold deposit

    黄铁矿呈稀疏浸染状、星点状分布于毒砂–黄铁绢英岩型矿石中。早世代黄铁(Py-1)矿呈浅黄色–黄白色中粗粒他形晶,大小为100~1000 μm,孔隙与裂纹极为发育,边部多被针柱状毒砂交代浸蚀(图4a);背散射电子图像呈暗色,内部结构较均一(图4b)。晚世代黄铁矿(Py-2)呈黄白色自形–半自形五角十二面体,含量少且颗粒小,大小为50~100 μm,内部结构均匀;多独立产出,其内部可见自形毒砂(图4c图4d)。

    辉锑矿(Stb)呈斑杂状、细脉状赋存于石英–辉锑矿脉型矿石中,具白色–灰白色半自形针柱状、粒状晶,大小为20~800 μm,易磨光且常见擦痕(图4e);白铁矿和锑氧化物多沿内部或边部交代辉锑矿(图4f图4h)。

    白铁矿(Mrc)含量较少,仅见于石英–辉锑矿脉型矿石中,以浅黄白色的密集条纹切面为鉴定特征,板柱状自形晶的大小为20~200 μm;大多以交代辉锑矿形式产出,少数独立赋存于石英中(图4f);背散射电子图像呈暗色的均质结构(图4g)。

    不同成矿期次的矿物组合特征差异明显:热液成矿期Ⅰ阶段为微细浸染状毒砂+黄铁矿+石英+绢云母组合,其中微晶石英粒径大小为50~200 μm,绢云母含量较高(20%~25%)且强烈定向排列(图3j);Ⅱ阶段金属矿物主要为辉锑矿+白铁矿,含微量早世代黄铁矿与毒砂,绢云母(5%~10%)呈较强的定向排列(图3k);Ⅲ阶段以无矿的方解石+石英+少量绢云母组合为特征,几乎不含金属硫化物,绢云母含量低(2%~5%)且无定向(图3l)。原生硫化物经浅表氧化淋虑,多形成黄锑矿+锑华+褐铁矿的表生期氧化矿物组合。主要矿物生成顺序见图5

    图  5  金盆梁金矿床矿物生成顺序图
    Figure  5.  Paragenetic sequence of the Jinpenliang gold deposit

    金盆梁金矿床载金硫化物的电子探针分析结果见表2

    表  2  金盆梁金矿床载金硫化物电子探针分析结果表(%)
    Table  2.  EMPA data (%) of Au–bearing sulfides in the Jinpenliang gold deposit
    测点号矿物AuSPbBiAgCdSbTeSeAsZnCuNiCoFeMnTiTotal计算化学式
    JPL-gb6-1毒砂
    (Apy)
    19.490.030.1046.050.090.020.050.0335.120.040.04101.06Fe1.03As1.01S
    JPL-gb6-220.860.030.7943.050.0035.480.030.00100.24Fe0.98As0.88S
    JPL-gb6-30.1019.990.030.3344.330.0335.550.01100.36Fe1.02As0.95S
    JPL-gb6-60.0319.440.020.060.0945.440.070.0835.410.03100.68Fe1.05As1.00S
    JPL-gb6-80.1319.210.060.5345.550.020.1035.62101.21Fe1.06As1.01S
    JPL-gb6-100.4719.920.0644.310.010.070.030.0935.50100.45Fe1.02As0.95S
    JPL-gb6-110.1619.440.150.010.0145.660.020.100.0935.73101.36Fe1.06As1.01S
    JPL-gb6-130.0320.530.060.060.070.9943.590.030.050.0535.520.010.03101.03Fe0.99As0.91S
    JPL-gb6-1619.810.020.050.5544.270.000.110.000.0735.44100.33Fe1.03As0.96S
    JPL-gb6-1819.550.050.050.010.6144.690.010.0435.63100.65Fe1.05As0.98S
    JPL-gb6-190.0320.430.010.7843.570.010.0535.160.03100.07Fe0.99As0.91S
    JPL-gb6-4早世代
    黄铁矿
    (Py-1)
    52.370.040.020.020.010.070.1447.180.0299.86Fe0.52S
    JPL-gb6-70.0551.610.011.750.0946.59100.09Fe0.52S
    JPL-gb6-951.390.140.050.030.060.110.110.030.0947.040.0099.05Fe0.53S
    JPL-gb6-140.3052.140.040.000.010.060.050.260.0546.250.0299.18Fe0.51S
    JPL-gb6-1552.550.010.020.040.200.1546.770.0299.75Fe0.51S
    JPL-gb6-5晚世代
    黄铁矿
    (Py-2)
    52.310.011.180.060.0546.1299.74Fe0.51S
    JPL-gb6-1251.950.010.060.700.040.1246.590.0399.50Fe0.51S
    JPL-gb6-1752.180.120.030.010.450.060.010.0447.010.0199.91Fe0.52S
    JPL-gb6-200.2550.673.040.130.050.0446.02100.21Fe0.52S
    JPL-gb5-1辉锑矿
    (Stb)
    27.270.0171.580.090.050.040.000.0599.10Sb0.69S
    JPL-gb5-428.660.150.0371.030.040.070.050.04100.06Sb0.65S
    JPL-gb5-50.2627.640.0971.080.110.010.020.000.0099.22Sb0.68S
    JPL-gb5-728.680.170.120.0371.050.010.120.03100.20Sb0.65S
    JPL-gb4-128.320.130.030.0270.920.040.010.090.060.020.000.030.0199.69Sb0.66S
    JPL-gb4-428.9871.520.020.160.030.02100.74Sb0.65S
    JPL-gb4-527.360.400.0771.890.060.090.030.070.130.060.00100.16Sb0.69S
    JPL-gb4-60.2927.970.0271.240.010.160.090.010.0199.79Sb0.67S
    JPL-gb4-90.0428.900.120.0670.780.020.210.050.060.01100.24Sb0.64S
    JPL-gb4-1029.030.0671.020.070.010.110.070.040.010.01100.43Sb0.64S
    JPL-gb4-1128.730.010.0470.490.120.110.0499.54Sb0.65S
    JPL-gb4-120.1528.310.030.0771.260.000.000.110.030.000.010.040.02100.04Sb0.66S
    JPL-gb4-2白铁矿
    (Mrc)
    0.1652.840.200.170.120.1646.490.03100.18Fe0.51S
    JPL-gb4-30.0552.610.090.060.011.270.000.110.020.150.1246.490.020.00100.98Fe0.51S
    JPL-gb4-70.1448.730.010.004.540.010.030.050.2241.1994.90Fe0.49S
    JPL-gb4-848.140.023.880.010.020.090.2241.430.0493.86Fe0.49S
    JPL-gb5-30.0752.970.010.250.020.040.130.2445.8799.61Fe0.50S
    JPL-gb5-652.270.130.090.1445.5698.19Fe0.50S
    JPL-gb5-80.0752.570.080.090.030.040.080.1745.890.0599.06Fe0.50S
    JPL-gb5-953.650.030.000.010.070.160.0946.800.01100.83Fe0.50S
     注:“−”表示低于检出限。
    下载: 导出CSV 
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    毒砂中7个测点(共11个)的Au含量高于检出限,占测点总数的63.64%。主元素组成较为稳定:Fe含量为35.12%~35.73%(平均值为35.47%),As含量为43.05%~46.05%(平均值为44.59%),S含量为19.21%~20.86%(平均值为19.88%)。计算分子式为FeAs0.90S1.02~FeAs0.98S0.97,接近于毒砂理想分子式FeAs1-xS1+xx ≤ |0.13|)(Sharp et al.,1985),且原子个数比S/As值为0.99~1.13,总体具有富As、低S与Fe的特征,指示毒砂的形成温度较高(Sharp et al.,1985员媛娇等,2022)。元素的相关性分析证实,S与As原子百分数呈明显的线性负相关(图6a),而S与Fe、Fe与As之间不存在显著的相关性(图6b、图6c),暗示可能存在As替代部分S进入毒砂晶格(沈关文等, 2022)。除Fe、As、S元素外,多数测点还含有Au(0~0.47%)、Ag(0~0.06%)、Cd(0~0.07%)、Sb(0~0.99%)、Zn(0~0.09%)、Co(0~0.10%)等微量元素,Au与As、S无明显相关性(图6g、图6h);Pb、Bi、Cu、Ni、Mn、Ti含量极低,仅个别测点高于检出限,Te、Se含量均低于检出限。

    图  6  金盆梁金矿床载金硫化物的元素关系图
    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Stb. 辉锑矿;Mrc. 白铁矿
    Figure  6.  Relationships between selected elements of Au–bearing sulfides in the Jinpenliang gold depoist

    黄铁矿中3个测点(共9个)Au含量高于检出限(0.05%~0.30%),占总测点数的33.33%。不同世代的黄铁矿主元素组成无显著差别:Py-1的S、Fe平均含量分别为52.01%、46.76%,原子个数比S/Fe值为1.90~1.96(平均值为1.94),计算化学式为Fe0.51S~Fe0.53S;Py-2的S、Fe平均含量分别为51.78%和46.43%,S/Fe值为1.92~1.98(平均值为1.94)且化学式为Fe0.51S~Fe0.52S(表2);与黄铁矿的理论值(S=53.45%,Fe=46.55%,原子个数比S/Fe=2)相比较,具有亏损S、略亏损或富集Fe的特征。所有测点的As含量均高于检出限,但Py-2中As含量(As=0.45%~3.04 %,平均值为1.34%)明显高于Py-1(As=0.01%~1.75%,平均值为0.37%),As–S–Fe三者之间无显著的相关性(图6d~图6f)。对比微量元素,Py-1中Ag(0~0.05%)、Pb(0~0.14%)、Zn(0~0.11%)、Co(0.05%~0.15%)、Ni(0~0.26%)略含量高于Py-2(Ag=0~0.01%,Pb=0~0.12%,Zn=0~0.06%,Co=0.04%~0.12%,Ni=0~0.05%),其他元素如Bi、Cd、Sb、Se、Mn、Ti仅个别测点高于检出限,Te含量均低于检出限。

    辉锑矿的4个测点(共12个)Au含量高于检出限(0.04%~0.29%),占比33.33%。S和Sb含量分别为27.27%~29.03%(平均值为28.32%)和70.49%~71.89%(平均值为71.15%),原子个数比S/Sb值为1.45~1.55,计算化学式Sb0.64S~Sb0.69S;与辉锑矿的理论值(S=28.62%,Sb=71.38%)相比,略亏损主元素S、Sb。辉锑矿中普遍含As,含量为0.07%~0.21%,平均值为0.12%。元素关系图显示,S与Sb呈较弱的负相关关系,As与S、Sb、Au无显著相关性(图6d~图6h)。微量元素中,Pb、Bi、Ag、Se、Zn、Co、Mn、Ti等元素含量较低,只有少部分测点高于检出限;而多数测点的Cd(0~0.07%)、Te(0~0.12%)、Cu(0~0.07%)、Ni(0~0.13%)、Fe(0~0.04%)含量高于检出限。

    白铁矿与黄铁矿互为同质多像变体(赵珊茸等,2004),两者具有相同的化学式和化学组成(FeS2,S=53.45%,Fe=46.55%)。作为金盆梁金矿的主要载金硫化物之一,白铁矿8个测点(共11个)Au含量高于检出限(0.05%~0.16%),占测点总数的72.73%。S、Fe含量分别为48.14%~53.65%(平均值为51.72%)和41.19%~46.80%(平均值为44.97%);原子个数比S/Fe值为1.97~2.06,平均值为2.00,显著贫S、Fe且二者呈线性正相关关系(图6e)。多数白铁矿测点含Cd(0~0.08%)、Sb(0~4.54%)、Se(0~0.03%)、As(0~0.11%)、Zn(0~0.17%)、Co(0.12%~0.24%)、Ni(0~0.16%)、Mn(0.12%~0.24%)等微量元素;仅个别测点的Bi、Cu、Ti含量高于检出限,Pb、Te含量均低于检出限。

    金的赋存状态是指金在矿石中的存在形式,以粒度划分的可见金(>0.1 μm)与不可见金(≤0.1 μm)是目前主流划分方案(张博等,2018)。前者包括明金、显微–次显微金等,可利用光学显微镜或扫描电镜观察;晶格金和纳米金等不可见金则往往难以观察(Cook et al.,1990)。金盆梁金矿床同一载金硫化物的电子探针数据中(表2),Au含量均存在高于和低于检出限且无异常高值点,高倍光学显微镜及背散射电镜下也未发现自然金颗粒,证明金可能主要以“不可见金”形式赋存于载金硫化物中。

    大量研究表明,“不可见金”在含砷黄铁矿、毒砂及白铁矿等硫化物中主要有2种赋存形式,即次显微–纳米级自然金Au0和晶格金Au+Fleet et al.,1993Simon et al.,1999a1999bCabri et al.,2000Palenik et al.,2004Reich et al.,2005Liang et al.,2021),晶格金Au李九玲等,2002)和Au3+Wu et al.,1989Arehart et al.,1993)尚有报道。金的赋存状态与黄铁矿颗粒大小存在关联,Simon等(1999a)对美国内华达Twin Creeks卡林型金矿区含砷黄铁矿的研究表明,粗粒含砷黄铁矿中以化学吸附作用的晶格金AuⅠ+为主,细粒含砷黄铁矿中金多呈次显微自然金Au0存在;由此推断,金盆梁金矿早世代粗粒黄铁矿的金赋存状态主要为晶格金Au+,白铁矿与晚世代细粒黄铁矿为次显微–纳米级自然金Au0。在Fe–As–S三角关系图上,黄铁矿和白铁矿中As含量较低,投点接近于理想组成(图7a)(Fleet et al.,1997);毒砂的投点大致平行于S–As轴(图7b),证明As替代S进入毒砂的晶格(Deditius et al.,2008Su et al.,2012),也为晶格金(固溶体金)的富集创造了先决条件(赵静等,2017)。Reich等(2005) 提出固溶体金在含砷黄铁矿中的最大溶解度曲线:CAu=0.02×CAs+4×10−5,可用于判别含砷黄铁矿和毒砂中金的赋存状态;落于该曲线上方区域的样品点(Au/As>0.02),金主要以纳米金Au0形式赋存,反之(Au/As<0.02)则以晶格金Au+为主。本研究毒砂、黄铁矿及白铁矿的数据投点分布于溶解度曲线两侧(图8),说明不同矿物中金的赋存状态差异显著:毒砂中的金均以晶格金Au+形式存在;早世代他形中粗粒黄铁矿含纳米金Au0和晶格金Au+;晚世代细粒自形黄铁矿和白铁矿的金为纳米金Au0

    图  7  金盆梁金矿床毒砂、黄铁矿及白铁矿Fe–As–S三角关系图
    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Mrc. 白铁矿
    Figure  7.  Ternary Fe–As–S diagrams of gold–bearing sulfides in the Jinpenliang gold deposit
    图  8  金盆梁金矿床毒砂、黄铁矿及白铁矿Au–As关系图(拟合曲线据Reich et al.,2005
    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Mrc. 白铁矿
    Figure  8.  Correlation of Au–As values in arsenopyrite, pyrite, and marcasite from the Jinpenliang gold deposit

    晶格金在毒砂和砷黄铁矿中的替代机制主要存在以下4点不同认识。①Au+占据砷黄铁矿晶格缺陷的阳离子空位(Fleet et al.,1997Simon et al.,1999a)。②未知Au–AsS化合物,Au+以四面体配位与硫和砷原子结合(Simon et al.,1999aReich et al.,2005)。③As替代S进入黄铁矿或毒砂内造成晶格错位和扭曲(Fougerouse et al.,2021),Au+/Au3+占据Fe2+的位置(Arehart et al.,1993Simon et al.,1999aSu et al.,2012)。④Au占据毒砂和含砷黄铁晶格中[AsS]3–的S的位置(李九玲等,2002)。金盆梁金矿床仅毒砂中的金以晶格金Au+为主,As替代S进入毒砂晶格(图6a图7a)且Au与Fe含量具弱正相关(剔除Au异常高值点0.47%,相关系数R2=0.34),指示Au+主要占据晶格畸变区Fe2+的位置。

    鉴于毒砂相对难熔且固溶体对于温度极为敏感,Kretschmar等(1976)首次提出可通过Fe–As–S矿物共生关系与毒砂的化学组成,来限定毒砂的形成温度和硫逸度。经Sharp等(1985)重新验证后,毒砂地质温度计被广泛应用于各类热液矿床的研究中(Choi et al.,2000Lentz,2002汪超等,2021)。金盆梁金矿床早阶段的金属矿物共生组合为毒砂–黄铁矿,将毒砂As原子百分数投于Fe–As–S相图的相应区域,可获取其形成时的物理化学参数。利用电子探针数据计算可得,毒砂的As原子百分数为31%~33%,估算出成矿早阶段(Ⅰ)毒砂的形成温度t为370~490 ℃,硫逸度logf(S2)为−8.5~−4.5(图9)。

    图  9  毒砂地质温度计的logf(S2)–t图解(据Sharp et al.,1985Zhang et al.,2018
    Apy. 毒砂;Py. 黄铁矿;Po. 磁黄铁矿;Lo. 斜方砷铁矿
    Figure  9.  Logf(S2) vs. t equilibria diagram of arsenopyrite geothermometer

    黄铁矿中的微量元素特征比值与含量变化,主要受控于沉淀时的物理化学条件和含矿热液的介质成分(胡楚雁,2001刘仕玉等,2021)。Co/Ni值是判别黄铁矿成因的重要标志(Loftus-Hills et al.,1967Bralia et al.,1979沈关文等,2022)。前人研究认为,沉积成因黄铁矿Co、Ni含量普遍较低且Co/Ni<1;热液成因黄铁矿的Co/Ni值相对较高(1<Co/Ni<5);火山成因黄铁矿Co/Ni>5,通常大于10(Bralia et al.,1979)。金盆梁金矿床黄铁矿和白铁矿的Co/Ni值为0.20~4.10,且普遍大于1(图6i),均属于热液成因。

    黄铁矿的微量元素组合与Co含量,可以反映矿床的形成环境(刘英俊等,1991张然等,2022)。通常高温条件下的黄铁矿富Cr、Ti、Co、Ni、Mo、Bi、Cu、Zn等亲铁和亲石元素,Co含量高于1000×10−6;中温环境中的黄铁矿含较多Au、Ag、Cu、Pb、Zn等亲铜元素,Co含量为100×10−6~1000×10−6;低温环境下的黄铁矿以富Hg、Sb、As、Ag等高活动性亲铜元素为特征,Co含量低于100×10−6。金盆梁金矿床早世代黄铁矿的Ag、Pb、Zn、Co及Ni含量略高于晚世代黄铁矿,Co含量分别为0.05%~0.15%和0.04%~0.12%,说明两者均形成于中高温环境,且早世代黄铁矿的形成温度略高于晚世代。Fe/(S+As)值与黄铁矿的形成深度相关系数高达0.87,深成、中成及浅成环境黄铁矿的上述比值分别约为0.846、0.863和0.926(周学武等,2005);金盆梁金矿黄铁矿的Fe/(S+As)值为0.857~0.914,平均值为0.885,主体形成于中浅成环境。

    由于金的溶解度随温度的升高略增大(Shenberger et al.,1989),综合矿物共生关系、金的赋存状态及毒砂地质温度计等的研究,可限定金盆梁金矿床主体形成于硫逸度logf(S2)为−8.5~−4.5的中高温、中浅成环境;从早至中阶段,成矿流体由较高温的相对自然金不饱和状态,逐渐演化为较低温的自然金饱和状态。

    南秦岭金盆梁金矿床的成矿背景、矿床地质特征、矿石特征、矿物共生组合、金的赋存状态及矿床地球化学特征等,与卡林型金矿床相似(Hofstra et al.,2000),显著区别于造山型(Groves et al.,1998Gu et al.,2023)和类卡林型金矿床(刘家军等,2019)。具体包括:①大地构造位置处于南秦岭晚古生带弧前盆地;赋矿岩系为泥盆系浅海–滨海相的碎屑–沉积岩建造,硅化粉砂质板岩为主要含矿岩性。②矿区夹持于印支期柞水和曹坪花岗岩基之间,与后者空间关系密切。③矿体以微细浸染型矿化蚀变岩为主,赋存于近东西向的高角度左行韧性剪切断层。④围岩蚀变类型包括硅化、毒砂–黄铁矿化、绢云母化和碳酸盐化。⑤成矿早期矿物组合为浸染状毒砂+黄铁矿+石英+绢云母,晚期为辉锑矿+白铁矿+石英+绢云母。⑥金以纳米级自然金Au0和晶格金Au+形式赋存于毒砂、黄铁矿及白铁矿中,Au+主要替代毒砂晶格中Fe2+。⑦成矿元素为Au–Ag–As–Sb中低温元素组合。⑧矿床形成于中高温的中浅成环境,成矿流体以大气降水为主(流体包裹体以气液两相水溶液型为主)。⑨热液方解石C、O同位素主要源于海相碳酸盐的溶解(δ13CV-PDB=–2.61‰~0.07‰,δ18OV-SMOW=15.83‰~16.45‰);矿石S来源于赋矿围岩(δ34S=–12.50‰~–10.20‰),Pb属于上地壳铅(未发表数据)。

    因而,对比美国内华达与南秦岭地区典型卡林型金矿床的地质特征与成矿条件(陈衍景等,2004Cline et al.,2005Ma et al.,2020),笔者认为金盆梁金矿的成因类型应归属于卡林型金矿。

    (1)金盆梁金矿床热液成矿期的金矿化以微细浸染型为主,可划分为3个成矿阶段:黄铁矿–毒砂–硅化阶段(Ⅰ )、石英–辉锑矿–白铁矿±锑氧化物阶段(Ⅱ)及方解石–石英阶段(Ⅲ)。近矿围岩蚀变以硅化、绢云母化、毒砂–黄铁矿化为主,远矿则主要为碳酸盐化。

    (2)金的赋存状态在不同的Fe–As–S载金矿物中存在差异,由毒砂中的晶格金Au+,到早世代黄铁矿中的晶格金Au+和纳米金Au0,至晚世代黄铁矿和白铁矿的纳米金Au0

    (3)金属矿物组合由毒砂–黄铁矿至辉锑矿–白铁矿,成矿流体从较高温的相对自然金不饱和状态,逐渐演化为较低温的自然金饱和状态。金盆梁金矿形成于硫逸度logf(S2)为–8.5~–4.5的中高温、中浅成环境,成因类型应归属于卡林型金矿床。

    致谢:野外工作得到了柞水县巨力多金属矿业开发中心的支持与帮助,成文过程中匿名审稿人提供了宝贵的修改意见,在此一并致谢!

  • 图  1   秦岭造山带构造单元(a)及柞水–山阳矿集区地质图(b)(据Ding et al.,2022修改)

    1. 第四系;2. 石炭系;3. 泥盆系;4. 下古生界;5. 前寒武系;6. 晚侏罗—早白垩世花岗岩;7. 中—晚三叠世花岗岩;8. 新元古代花岗岩;9. 新元古代闪长岩;10. 辉长–辉绿岩;11. 角闪岩;12. 卡林型金矿床;13. 热水沉积改造型银矿床;14. 热水沉积改造型铜矿床;15. 热水沉积改造型铁矿床;16. 岩浆分结型铁矿床;17. 矽卡岩–斑岩型铜矿床;18. 断层;19. 地质界线;20. 地名

    Figure  1.   (a) Tectonic framework of the Qinliong orogen and (b) geological map of the Zhashui–Shanyang ore district cluster

    图  2   金盆梁金矿床地质图(据苏选民等,2012

    1. 下石炭统二峪河组上亚组下段;2. 下石炭统二峪河组下亚组上段;3. 上泥盆统(未分);4. 上泥盆统桐峪寺组第六岩性段;5. 上泥盆统桐峪寺组第五岩性段上亚段;6. 上泥盆统桐峪寺组第五岩性段下亚段;7. 上泥盆统桐峪寺组第四岩性段上亚段;8. 二长花岗岩;9. 闪长玢岩脉;10. 云斜煌斑岩脉;11. 矿体及编号;12. 矿化体;13. 断层及编号;14. 地名

    Figure  2.   Geological map of the Jinpenliang gold deposit

    图  3   金盆梁金矿床典型矿体与矿石照片

    a. 主矿体赋存于粉砂质板岩的断裂中,石英–辉锑矿细脉切穿毒砂–黄铁矿化蚀变岩;b. 受左行韧性剪切作用,石英–辉锑矿脉呈浅黄色透镜状产出;c. 矿体远端的方解石–石英脉;d. 毒砂–黄铁绢英岩型矿石;e. 石英–辉锑矿脉型矿石;f. 方解石–石英脉手标本;g. 毒砂、黄铁矿呈微细浸染状,见自形毒砂沿边部交代他形粗粒黄铁矿;h. 辉锑矿呈半自形晶,含少量白铁矿;i. 方解石细脉切穿粗粒石英;j-l. Ⅰ~Ⅲ阶段的非金属矿物特征;Py. 黄铁矿;Apy. 毒砂;Stb. 辉锑矿;Mrc. 白铁矿;Q. 石英;Cal. 方解石;Ser. 绢云母

    Figure  3.   Photos of typical orebodies and ores of the Jinpenliang gold deposit

    图  4   金盆梁金矿石硫化物显微特征图

    a~d. 毒砂沿早世代黄铁矿边部或内部交代,构成毒砂–黄铁矿聚合体,见晚世代黄铁矿包含自形细粒毒砂;e~g. 辉锑矿呈自形–半自形粒状,白铁矿和锑氧化物交代辉锑矿;h~i. 黄锑矿和白铁矿的能谱图;Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Stb. 辉锑矿;Mrc. 白铁矿;Cvn. 黄锑矿;Q. 石英

    Figure  4.   Microscopic characteristics of sulfides in ores of the Jinpenliang gold deposit

    图  5   金盆梁金矿床矿物生成顺序图

    Figure  5.   Paragenetic sequence of the Jinpenliang gold deposit

    图  6   金盆梁金矿床载金硫化物的元素关系图

    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Stb. 辉锑矿;Mrc. 白铁矿

    Figure  6.   Relationships between selected elements of Au–bearing sulfides in the Jinpenliang gold depoist

    图  7   金盆梁金矿床毒砂、黄铁矿及白铁矿Fe–As–S三角关系图

    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Mrc. 白铁矿

    Figure  7.   Ternary Fe–As–S diagrams of gold–bearing sulfides in the Jinpenliang gold deposit

    图  8   金盆梁金矿床毒砂、黄铁矿及白铁矿Au–As关系图(拟合曲线据Reich et al.,2005

    Apy. 毒砂;Py-1. 早世代黄铁矿;Py-2. 晚世代黄铁矿;Mrc. 白铁矿

    Figure  8.   Correlation of Au–As values in arsenopyrite, pyrite, and marcasite from the Jinpenliang gold deposit

    图  9   毒砂地质温度计的logf(S2)–t图解(据Sharp et al.,1985Zhang et al.,2018

    Apy. 毒砂;Py. 黄铁矿;Po. 磁黄铁矿;Lo. 斜方砷铁矿

    Figure  9.   Logf(S2) vs. t equilibria diagram of arsenopyrite geothermometer

    表  1   金盆梁金矿床矿石类型与硫化物特征表

    Table  1   Ore types and sulfide characteristics of the Jinpenliang gold deposit

    矿石类型金属硫化物特征描述素描图
    毒砂–黄铁绢英岩型 Apy 毒砂(Apy)呈亮白色针柱状、菱形、茅状自形晶,常见晶面裂纹与孔隙;呈独立放射状或沿早世代黄铁矿边部交代形成毒砂–黄铁矿集合体

    Py-1 早世代黄铁矿(Py-1)呈浅黄色–黄白色中粗粒他形晶,孔隙与裂纹发育;内部结构均一,增生环带不明显,边部多被自形–半自形毒砂交代浸蚀
    Py-2 晚世代黄铁矿(Py-2)呈黄白色细粒自形–半自形晶,孔隙与裂纹较少,内部为均质结构;多独立产出,偶见内部包含自形毒砂颗粒
    石英–辉锑矿脉型 Stb 辉锑矿(Stb)反射色为白色–灰白色,多色性极为显著,多呈半自形针柱状、粒状晶,易磨光,常见擦痕。可见白铁矿、黄锑矿(Cvn)等交代辉锑矿
    Mrc 白铁矿(Mrc)呈浅黄白色自形板柱状晶,以似节理状的密集条纹切面为鉴别特征,大多沿辉锑矿边部或内部交代产出,极少数独立赋存于石英中
    下载: 导出CSV

    表  2   金盆梁金矿床载金硫化物电子探针分析结果表(%)

    Table  2   EMPA data (%) of Au–bearing sulfides in the Jinpenliang gold deposit

    测点号矿物AuSPbBiAgCdSbTeSeAsZnCuNiCoFeMnTiTotal计算化学式
    JPL-gb6-1毒砂
    (Apy)
    19.490.030.1046.050.090.020.050.0335.120.040.04101.06Fe1.03As1.01S
    JPL-gb6-220.860.030.7943.050.0035.480.030.00100.24Fe0.98As0.88S
    JPL-gb6-30.1019.990.030.3344.330.0335.550.01100.36Fe1.02As0.95S
    JPL-gb6-60.0319.440.020.060.0945.440.070.0835.410.03100.68Fe1.05As1.00S
    JPL-gb6-80.1319.210.060.5345.550.020.1035.62101.21Fe1.06As1.01S
    JPL-gb6-100.4719.920.0644.310.010.070.030.0935.50100.45Fe1.02As0.95S
    JPL-gb6-110.1619.440.150.010.0145.660.020.100.0935.73101.36Fe1.06As1.01S
    JPL-gb6-130.0320.530.060.060.070.9943.590.030.050.0535.520.010.03101.03Fe0.99As0.91S
    JPL-gb6-1619.810.020.050.5544.270.000.110.000.0735.44100.33Fe1.03As0.96S
    JPL-gb6-1819.550.050.050.010.6144.690.010.0435.63100.65Fe1.05As0.98S
    JPL-gb6-190.0320.430.010.7843.570.010.0535.160.03100.07Fe0.99As0.91S
    JPL-gb6-4早世代
    黄铁矿
    (Py-1)
    52.370.040.020.020.010.070.1447.180.0299.86Fe0.52S
    JPL-gb6-70.0551.610.011.750.0946.59100.09Fe0.52S
    JPL-gb6-951.390.140.050.030.060.110.110.030.0947.040.0099.05Fe0.53S
    JPL-gb6-140.3052.140.040.000.010.060.050.260.0546.250.0299.18Fe0.51S
    JPL-gb6-1552.550.010.020.040.200.1546.770.0299.75Fe0.51S
    JPL-gb6-5晚世代
    黄铁矿
    (Py-2)
    52.310.011.180.060.0546.1299.74Fe0.51S
    JPL-gb6-1251.950.010.060.700.040.1246.590.0399.50Fe0.51S
    JPL-gb6-1752.180.120.030.010.450.060.010.0447.010.0199.91Fe0.52S
    JPL-gb6-200.2550.673.040.130.050.0446.02100.21Fe0.52S
    JPL-gb5-1辉锑矿
    (Stb)
    27.270.0171.580.090.050.040.000.0599.10Sb0.69S
    JPL-gb5-428.660.150.0371.030.040.070.050.04100.06Sb0.65S
    JPL-gb5-50.2627.640.0971.080.110.010.020.000.0099.22Sb0.68S
    JPL-gb5-728.680.170.120.0371.050.010.120.03100.20Sb0.65S
    JPL-gb4-128.320.130.030.0270.920.040.010.090.060.020.000.030.0199.69Sb0.66S
    JPL-gb4-428.9871.520.020.160.030.02100.74Sb0.65S
    JPL-gb4-527.360.400.0771.890.060.090.030.070.130.060.00100.16Sb0.69S
    JPL-gb4-60.2927.970.0271.240.010.160.090.010.0199.79Sb0.67S
    JPL-gb4-90.0428.900.120.0670.780.020.210.050.060.01100.24Sb0.64S
    JPL-gb4-1029.030.0671.020.070.010.110.070.040.010.01100.43Sb0.64S
    JPL-gb4-1128.730.010.0470.490.120.110.0499.54Sb0.65S
    JPL-gb4-120.1528.310.030.0771.260.000.000.110.030.000.010.040.02100.04Sb0.66S
    JPL-gb4-2白铁矿
    (Mrc)
    0.1652.840.200.170.120.1646.490.03100.18Fe0.51S
    JPL-gb4-30.0552.610.090.060.011.270.000.110.020.150.1246.490.020.00100.98Fe0.51S
    JPL-gb4-70.1448.730.010.004.540.010.030.050.2241.1994.90Fe0.49S
    JPL-gb4-848.140.023.880.010.020.090.2241.430.0493.86Fe0.49S
    JPL-gb5-30.0752.970.010.250.020.040.130.2445.8799.61Fe0.50S
    JPL-gb5-652.270.130.090.1445.5698.19Fe0.50S
    JPL-gb5-80.0752.570.080.090.030.040.080.1745.890.0599.06Fe0.50S
    JPL-gb5-953.650.030.000.010.070.160.0946.800.01100.83Fe0.50S
     注:“−”表示低于检出限。
    下载: 导出CSV
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  • 收稿日期:  2023-02-08
  • 修回日期:  2023-06-10
  • 网络出版日期:  2023-07-19
  • 刊出日期:  2023-10-19

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