Discussion on the ore-controlling factors in the Longlin–Xilin Sb–Au mining district of western Guangxi, South China
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摘要: 华南锑成矿省锑资源储量占全国83%以上，位于成矿省西南部的滇黔桂锑矿带是华南锑成矿省的重要组成部分。文章以滇黔桂锑矿带中部桂西隆林−西林锑金矿集区为例，系统分析了区内82个矿床（点）的赋矿层位、赋矿围岩岩性、容矿构造特征及锑、金矿床共伴生关系，结合3个典型矿床调查及岩浆岩时空分布，探讨锑成矿作用与碎屑岩、岩浆岩的成因联系。研究结果表明：具有高锑背景值的炭质泥页岩和富黄铁矿砂岩是研究区锑成矿的有利岩性，为锑成矿提供了物质来源。岩浆作用对锑成矿既可以起到直接作用（Sb和S来源）也可以起到间接作用（热源），两者均有利于锑矿床的形成。容矿构造分析显示研究区经历了印支期南北向挤压，随后叠加中晚侏罗世北西—南东向挤压。北西西—南东东向和北东—南西向断裂及其交汇处是有利的容矿空间。隆林−西林矿集区锑、金矿床统计显示，区内以独立的锑、金矿床为主，暗示研究区锑、金成矿流体可能多为不同来源流体。在上述研究基础上，文章提出桂西隆林－西林锑金矿集区勘查有利区域：新州背斜核部下泥盆统郁江组炭质泥页岩和富黄铁矿粉砂岩是锑矿勘查的重点层位；隆林县弄桑−石家寨北西西—南东东向断裂带内隐伏岩体周边和西林县北西西—南东东向斗皇−西林断裂与北东—南西向断裂的交汇部位是锑矿勘查的有利区域。以上成果为研究区内锑金矿床成因和成矿规律认识提供新的思考，为区内锑矿床勘查提供方向。Abstract:
Objective Sb deposits are characterized by simple mineral assemblage. The ore-forming ages, sources of ore-forming materials, and genesis of Sb deposits are controversial owing to the absence of suitable minerals for analysis. Sb resources in the South China Sb metallogenic region account for over 83% of the national total, with the Dian–Qian–Gui Sb belt in the southwest being an significant component of this region. Methods Taking the Longlin–Xilin Sb–Au mining district of western Guixi in the central part of the Dian–Qian–Gui Sb belt as an example, this paper systematically summarizes the ore-bearing strata, lithology of ore-bearing wall rocks, ore-bearing structures, and the coexistence relationship of Au and Sb deposits in 86 ore deposits (points) in the area. Combined with the geological characteristics of three typical deposits (Maxiong, Longtan, and Mahao) and the spatiotemporal distribution of Jurassic felsic intrusions, the inherent connection between Sb mineralization and clastic rocks and felsic intrusions was explored. Results (1) Statistics and field works show that the most favorable ore-bearing stratum in the Longlin–Xilin mining district is the Lower Devonian Yujian Formation (D1y) , followed by the Lower Triassic Luolou Formation (T1Ll) and the Middle Triassic Banna Formation (T2b). The lithologies most conducive to mineralization are carbonaceous shale, pyrite-rich sandstone, and siltstone. The Sb content in these strata or lithologies is tens or even hundreds of times higher than the crustal abundance, which has the potential for Sb mineralization. (2) Within the NWW–SEE trending Nongsang–Shijiazhai fault zone in the Longlin area, the middle and late Jurassic felsic intrusions, which have consistent spatiotemporal occurrences with Sb and Au deposits, can directly contribute to antimony mineralization (as sources of Sb and S) and indirectly influence it (as a heat source), both favoring the formation of antimony deposits. (3) Statistical results show that Sb, Au, and Sb–Au deposits account for 48%, 46%, and 6% in the Longlin–Xilin district, respectively. This suggests that the ore-forming fluids for Sb and Au in the study area may originate from different sources. We also can not rule out the possibility that Sb and Au deposits derive from the same fluid. In the latter case, the precipitation of stibnite consumes H2S in the ore-forming fluid, destabilizing the Au complex in the solution and resulting in localized Au precipitation. This competition between Sb and Au in the fluid for H2S leads to a negative correlation in the grades of Sb and Au in coexisting deposits. (4) The study area experienced NS-striking compression in the Indosinian period, followed by the NW–SE shortening in the middle–late Jurassic. The intersection of NWW–SEE and NE–SW faults is the favorable ore-bearing space. The NWW–SEE faults displayed strike-slip movement in response to the NW–SE shortening, whereas the NE–SW faults exhibited transpression. Consequently, the NE–SW faults are less conducive to Sb mineralization compared to the NWW–SEE faults. The distribution direction of the NWW–SEE Douhuang–Xilin fault aligns with the axial direction of the main folds in the area, with most fault planes trending northward, displaying horizontal scratches, silicification, and extensional characteristics. The intersection of the Dohuang–Xilin fault and the NE–SW fracture exhibits significant Sb anomalies. Conclusion Based on the above studies, the promising areas we propose for Sb prospecting in Longlin–Xilin mining district are (1) Black shale and pyrite-rich siltstones of the Yujiang Formation in the core of the Xinzhou anticline as the key strata; (2) The periphery of the concealed intrusions within the NWW–SEE Nongsang–Shijaizhai fault (Longlin County) and the intersection area of the NWW–SEE Douhuang–Xilin fault and the NE–SW fault as the favorable areas. [ Significance ] The findings provide new insights into the genesis and metallogenic regularities of Sb–Au deposits in the study area, enriching the theoretical understanding of Au mineralization processes. -
0. 引言
斑岩型矿床是世界上铜、钼和铼等金属最重要来源, 环太平洋地区是世界上最主要的斑岩铜矿带[1-2]，仅南美洲安第斯带的智利、秘鲁就拥有El Teniente，Chuquicamata、Río Blanco-Los Bronces、La Escondida、Los Pelambres-El Pachón、Rosario、Radomiro Tomic、El Salvador、Toki、La Granja、Cujaone、Cerro Casala、Minas Congas等众多千万吨以上的巨型斑岩铜(金)矿，探明储量超过2.6亿吨，占全球铜探明储量的37.7%，产量占全球铜产量的39%(世界矿产资源年评，2014)，其中El Teniente铜储量约为9千多万吨，且含金超过2500吨[2-7]。对安第斯带斑岩型矿床的研究，一直是地质学家研究的热点。
文章依托中国地质调查局“全球矿产资源信息系统”和有关项目，试图通过总结南美安第斯带斑岩型铜(金-钼)矿床的时空分布特征，为认识安第斯带斑岩型矿床成矿地质特征、成矿规律等提供参考。
1. 安第斯带斑岩型铜(金-钼)矿床时空分布
斑岩型矿床是南美安第斯带最重要的铜(金-钼)矿床类型。斑岩铜矿原指产于强烈绢云母化和石英化中酸性斑岩里的细脉浸染型铜矿，目前多数学者认为斑岩铜矿是指与花岗质斑状侵入岩相关的，且钾质硅酸盐蚀变普遍发育于岩体内部，岩浆期后热液形成的细脉浸染状和角砾状硫化物矿床，还包括部分矽卡岩矿体[8]，也包括与斑岩型矿床有密切时空和成因联系的叠加其上的浅成低温热液金银铜矿床[9]。
根据基底组成、构造-岩浆演化、板块俯冲形式和成矿作用的不同，安第斯造山带自北而南划分为3个次级构造单元，即：北安第斯带、中安第斯带和南安第斯带，北、中安第斯带构造分界约在5°S左右的厄瓜多尔的瓜亚基尔湾，中、南安第斯带构造分界为39°S左右的智利南部的瓦尔迪维亚(Valdivia)[10-11]。
在整个安第斯带上，斑岩型铜矿带长约6000 km，呈线性多条带状分布，与安第斯造山带平行(图 1)，每个斑岩铜成矿带的发育都受限于不同的成矿期[12]。从目前勘探和开发情况看，中安第斯段一直是铜矿勘探和开采的热点地区，特别是秘鲁南部—智利中北部和阿根廷西北部地区，发现了一大批具有巨型规模的斑岩铜矿; 北安第斯段的斑岩铜矿也逐渐受到重视，南安第斯段的斑岩铜潜力很小[1, 13]。
1.1 北安第斯段
明显分出三条斑岩铜矿带，北部主要分布在6°N~9°N之间，以哥伦比亚的Acandi、Pantanos-Pegadorcito、Murindo等为代表，成矿时代在48.7~42 Ma，属于始新世；向南(在5°N~5°S之间)形成大致与造山带平行的两条斑岩铜矿带，西侧以厄瓜多尔的Junin、Gaby-Papa Grande及秘鲁的Rio Blanco等为代表，成矿时代在中新世(20~6.5 Ma)；东侧以厄瓜多尔的Mirador、Panantza等为代表，成矿时代是中晚侏罗世(150~170 Ma)。
1.2 中安第斯段
1.2.1 秘鲁中北部(5°S~12°S之间)
该区存在一条长1200 km，宽50~100 km的斑岩型铜(金-钼)矿带，沿西科迪勒拉延伸，成矿时代为中新世-上新世(20~5 Ma)。该带著名的巨型斑岩铜(金-钼)矿床有Toromocho、EI Galeno、Minas Conga及矽卡岩型铜(金)矿床Antamina。
1.2.2 秘鲁南部(12°S~18°S之间)
该区存在3条斑岩铜矿带，沿海岸科迪勒拉延伸的以Zafranal、Almacen、Anita de Tibilos等为代表，带宽在30 km左右，成矿时代为晚侏罗世—早白垩世(160~100 Ma)；第二条带分布在14°S~16°S之间，成矿时代是始新世晚期—渐新世(40~20 Ma)，以Las Bambas、Tintaya、Chalcobamba等为代表；第三条带分布在16°S~18°S之间，成矿时代为古新世(62~50 Ma)，这是秘鲁最著名的铜矿集中区，象Cuajone、Quellaveco、Toquepala、Cerro Verde/Santa Rosa等巨型斑岩矿床都分布在这里。
1.2.3 秘鲁南部—智利中北部(含阿根廷西北部)(12°S~39°S之间)
这是安第斯带斑岩型铜(金-钼)矿床发现数量多、分布相对最集中、矿床规模达巨型数量也最多的地段，有5条斑岩铜矿带，以古新世—早始新世带、中始新世—早渐新世带和中新世—早上新世带最为重要。
(1) 成矿时代最老(250~292 Ma)的斑岩铜矿出现在二叠纪，沿智利和阿根廷西部边界分布(20°S~40°S)，矿床规模不大。
(2) 中生代晚期(100~160 Ma)的斑岩铜矿发育在13°S~34°S的海岸科迪勒拉，断续延长2300 km，带宽在30 km左右，该带以众多铁氧化物型Cu-Au矿床和曼陀型(Manto)铜矿床为主，主要有Raul-Condestable、Manto verde和Michilla、Mantos Blancos、El Soldado、Lo Aguirre等。
(3) 古新世—早始新世(45~65 Ma)的斑岩铜矿主要产于16°S~32°S，位于西科迪勒拉西侧斜坡，铜矿带平均宽度为30~50 km。该带最著名的矿床有秘鲁的Cerro Verde-Santa Rosa、Cuajone、Quellaveco、Toquepala及智利的Cerro Colorado、Spence矿床，以高Mo，低Au为特征。
(4) 中始新世—早渐新世(45~30 Ma)的斑岩铜矿带从秘鲁南部的13°30′S向南一直延伸到智利北部31°S，全长约2500 km，在秘鲁南部带宽约130 km，在智利北部变为30~50 km宽，而在24.6°S的阿根廷西北部该带宽约150 km。在秘鲁南部矿带位于东、西科迪勒拉之间的坳陷地带，矿化与Andahuaylas-Yauri钙碱性岩基有时空关联，典型矿床有Antapaccay、Coroccohuayco、Tintaya、Los Chancas和Cotabarnbas等；在智利北部，从20°S~26°S之间，该带长>1000 km，产于Domeyko科迪勒拉，斑岩铜矿床位于Domeyko断裂系统之上或附近，受该断裂体系控制明显[15-18]，典型矿床有Chuquicamata、Potrerillos、EI Salvador、Escondida、Quebrada Blanca、Zaldivar、Radomiro Tomic、EI Abra等。
(5) 中新世-早上新世(23~4 Ma)的斑岩铜矿带位于智利中部—阿根廷中部之间，可细分三个亚带：智利中部亚带位于32°S~35°S之间，沿主科迪勒拉延伸约400 km，矿床形成时代约12~4 Ma，主要矿床有Los Pelambres、Rio Blanco-Los Bronces和EI Teniente；Maricunga-El Indio亚带位于智利中部亚带北部，26°S~31°S之间，矿床形成时代约12~4 Ma，以斑岩铜金矿为主，如Cerro Casale等；Farallon Negro亚带位于阿根廷西北部的安第斯山脉前陆地带，24°S~26°S之间，矿床形成时代约10~5 Ma，以斑岩铜(金-钼)矿为主，如Bajo dela Alumbrera、Agua Rica和Los Pelambres-El Pachon等。
在中安第斯段，从秘鲁南部—智利中部斑岩型铜(金-钼)矿床分布看，铜矿带的成矿时代具有向东逐渐年轻的倾向，这可能是由于在大陆边缘受一系列长期大洋板块俯冲作用的影响[19~21]。
从安第斯带斑岩型铜(金-钼)矿床时空分布看，矿床成矿时代大体可分为6期，其中，晚古生代冈瓦纳造山旋回2期：二叠纪(300~250 Ma)和中晚侏罗世(175~145 Ma)；中—新生代安第斯造山旋回4期：早白垩世(140~100 Ma)、古新世—始新世(65~50 Ma)、始新世晚期—渐新世(43~31 Ma)和中新世中期—上新世(12~4 Ma)。冈瓦纳造山旋回的两期斑岩铜矿化规模都较小，分布局限，其中，二叠纪的斑岩铜矿仅发育在智利东部和阿根廷西北部[19]；中晚侏罗世的斑岩铜矿主要发育在厄瓜多尔和哥伦比亚一带。
安第斯造山旋回是该区斑岩型铜矿形成的主要时期，最主要的是始新世晚期-渐新世(43~31 Ma)和中新世中期—上新世(12~4 Ma)时期，主要产在中安第斯段，以秘鲁南部—智利中北部(含阿根廷西北部)为主。
1.3 南安第斯段
该段中—新生代火山-岩浆活动强度比中安第斯段相对较弱，岩性多偏基性，以玄武质或玄武安山质为主[10]。成矿作用也与中安第斯段存在较大差异，基本没有斑岩型矿床存在[12]，矿床类型以浅成低温热液型的金、银矿床和喷流沉积型(Sedex)Zn-Pb-Ba-Ag多金属矿床为主。
2. 安第斯带斑岩型铜矿床形成时期
安第斯带已知斑岩铜矿床的铜资源量为5.9亿吨(表 1)，其中，始新世—渐新世形成的斑岩铜矿为2.69亿吨，约占已发现铜资源量的45.4%，中新世—上新世形成的斑岩铜矿为1.949亿吨，约占已发现铜资源量的32.9%，这两期形成的斑岩铜矿占已发现的全部铜资源量的78.3%，表明始新世—渐新世、中新世—上新世是南美最主要的2个斑岩铜矿形成时期。
表 1 安第斯带各斑岩铜矿成矿期已发现的铜资源量Table 1. Copper resources discovered during the ore-forming period of various porphyry copper deposits in the Andes belt成矿时代 铜资源量(万吨) 占已发现资源量的比例 新生代 中新世—上新世 19490 32.9% 渐新世—中新世 5110 8.6% 始新世—渐新世 26900 45.4% 古新世—始新世 6500 11.0% 中生代 早白垩世 155 0.3% 中晚侏罗世 900 1.5% 古生代 二叠纪 200 0.3% 合计 59255 100% 资料来源：USGS Open-File Report 2008-1253[22] 3. 结论
南美安第斯带是全球斑岩型铜(金-钼)矿床赋存最丰富的地区，矿带呈线性多条带状分布，与安第斯造山带平行。秘鲁中南部—智利中北部(含阿根廷西北部)为安第斯带斑岩型铜(金-钼)矿床发现数量最多、分布最集中、矿床规模达巨型数量最多的地段。斑岩矿床成矿时代有晚古生代冈瓦纳造山旋回两期和中—新生代安第斯造山旋回4期，以始新世晚期—渐新世和中新世中期—上新世最为重要。
致谢: 文章图件由中国地质大学(北京)硕士研究生郑瑜林清绘完成，在此深表谢意。 -
图 1 右江盆地区域地质图
a—研究区大地构造位置图（据胡丽娟等，2023修改）；b—右江盆地锑、金矿床分布图（据Xiao et al.，2022修改）
Figure 1. Regional geological map of the Youjiang basin
(a) Tectonic map of Asia showing continental blocks and bounding sutures (modified after Hu et al., 2023); (b) Distribution map of Sb–Au deposits in the Youjiang basin (modified after Xiao et al.，2022)
图 2 桂西隆林−西林锑金矿集区地质图
Figure 2. Geological map of the Longlin–Xilin Sb–Au district in western Guangxi
图 3 马雄锑矿床矿体及矿物特征
a—0号勘探线剖面图（据Yan et al.，2022修改）；b—主矿体顶部为炭质页岩；c—容矿北西西—南东东向走滑断裂底面水平擦痕产状特征（走滑断裂底面水平擦痕矢量数据反演显示三轴主应力方向σ1为351°/12°、σ2为110°/67°、σ3为256°/20°，指示近南北向挤压应力场）；d—脉状矿化的辉锑矿、石英和蚀变围岩中的黄铁矿；e—脉状矿化的辉锑矿、方解石、石英
Figure 3. Ore body and mineral characteristics of the Maxiong antimony deposit
(a) Geological cross-section along the exploration line 0 (modified after Yan et al.，2022); (b) The hanging wall of the main ore body composed of carbonaceous shales; (c) Occurrence characteristics of horizontal scratches on the bottom surface of NWW–SEE strike-slip ore-bearing fault (Inversion of horizontal scratches vector data on the bottom surface of strike-slip fault shows that the triaxial principal stress directions σ1 is 351°/12°, σ2 is 110°/67° and σ3 is 256°/20°, indicating the near NS compressive stress field); (d) Stibnite–quartz vein mineralization and pyrite in altered wall rocks; (e) Stibnite–quartz–calcite vein mineralization
图 4 龙滩锑矿床矿体及矿物特征
a—A12勘探线地质剖面图（据广西壮族自治区二七四地质队，1990修改）；b—层状矿体；c—脉状矿体产于北东东—南西西向高角度走滑断裂中(高角度走滑断裂断层面擦痕矢量数据反演显示三轴主应力方向σ1为129°/9°、σ2为28°/53°、σ3为226°/36°，指示北西—南东向挤压应力场)；d—方解石−辉锑矿矿石手标本；e—脉状矿化的辉锑矿、方解石
Figure 4. Ore body and mineral characteristics of the Longtan Sb deposit
(a) Geological cross-section along the exploration line A12 (modified after No.274 Team of Guangxi Bureau of Geology, 1990); (b) Stratiform ore body in Luolou Formation sandstones; (c) Vein ore bodies occur in NEE–SWW high angle strike-slip faults (Inversion of the vector data of scratches on the fault plane of high-angle strike-slip fault shows that the triaxial principal stress directions σ1 is 129°/9°, σ2 is 28°/53° and σ3 is 226°/36°, indicating that it was formed in the NW–SE compressive stress field); (d) Calcite–stibnite hand specimen; (e) Stibnite–calcite vein mineralization
图 5 马蒿锑矿床矿体及矿物特征
a—6号勘探线地质剖面图（据广西金果子矿业有限公司，2011修改）；b—马蒿锑矿床文洞矿段容矿断裂具有右行正断特征，金、锑矿体产在断裂下盘牵引褶皱核部虚脱空间；c—辉锑矿矿石手标本；d—辉锑矿−石英脉中石英与辉锑矿、黄铁矿共生
Figure 5. Ore body and mineral characteristics of the Mahao Sb deposit
(a) Geological cross-section along the exploration line 6 (modified after Guangxi Jinguozi Mining Co., Ltd, 2011); (b) The ore-bearing fault in Wendong ore segement of Mahao Sb deposit characterized by right-lateral normal faulting, with the Au (Sb) ore bodies occurring in the core space of traction folds formed by footwall of faults; (c) Stibnite hand specimen; (d) Stibnite coexisting with quartz and pyrite
图 6 桂西隆林−西林锑金矿床特征饼图
a—主要赋矿地层占比图；b—赋矿围岩岩性占比图；c—容矿断裂走向占比图；d—金、锑共伴生组合占比图
Figure 6. Pie charts of Sb-Au deposit in the Longlin–Xinlin mining district, western Guangxi
(a) Ore-bearing stratums; (b) Lithologies of ore-bearing rocks; (c) Ore-bearing faults; (d) Au and Sb co-existing assemblages
图 7 隆林县大树脚北西西—南东东向逆冲断层错断中二叠世玄武岩露头剖面及素描图
a—剖面图；b—素描图
Figure 7. The Outcrop profile and geologic sketch of Middle Permian basalt staggered by the NWW–SEE thrust fault in Dashujiao, Longlin County
(a) Outcrop profile; (b) Geologic sketch
图 8 隆林北西西—南东东向含矿断裂中锑、金矿床及长英质岩脉分布图
a—隆林北西西—南东东向含矿断裂中锑、金矿床及晚侏罗世长英质岩脉分布图；b—大树脚长英质岩脉侵入中二叠世玄武岩；c—弄桑长英质岩脉；d—石家寨长英质岩
Figure 8. Distribution map of antimony deposits, gold deposits, and felsic dikes in NWW–SEE striking faults in Longlin Country
(a) Distribution map of Sb deposit, Au deposits, and Late Jurassic felsic dikes in NWW–SEE ore-bearing faults; (b) Felsic dyke intruded into the Middle Permian basalt at Dashujiao, Longlin Country; (c) Felsic dyke occurred at Nongsang, Longlin Country; (d) Felsic rock occurred at Shijiazhai, Longlin Country
图 9 隆林−西林地区不同时代地层锑丰度
Є2—中寒武统；Є3—上寒武统；D3—上泥盆统；D1y—下泥盆统郁江组；D2d—中泥盆统东岗岭组；C—石炭系；C2—中石炭统；P1—下二叠统；P2—上二叠统；T1—下三叠统；T2—中三叠统；T2b—中三叠统板纳组；T2l—中三叠统兰木组a—隆林地区不同时代地层锑丰度（数据引自杨怀顺，2007）；b—三林地区不同时代地层锑丰度（数据引自韦文灼，1993）
Figure 9. Sb abundance in different strata in the Longlin–Xilin area
(a) Sb abundance in stratigraphic units of different ages in the Longlin area (data from Yang, 2007); (b) Sb abundance stratigraphic units of different ages in the Sanlin area (data from Wei, 1993)Є2–the Middle Cambrian; Є3–the Upper Cambrian; D3–the Upper Devonian; D1y–the Yujiang Formation of the Lower Devonian; D2d–the Donggangling Formation of the Middle Devonian; C–the Carboniferous; C2–the Middle Carboniferous; P1–the Lower Permian; P2–the Upper Permian; T1–the Lower Triassic; T2–the Middle Triassic; T2b–the Banna Formation of the Middle Triassic; T2l–the Mulan Formation of the Middle Triassic
表 1 国内外典型锑矿床赋矿围岩岩性
Table 1. Lithology of the surrounding rocks of typical antimony deposits at home and abroad
国家 地区 矿床名称 赋矿围岩主要岩性 参考文献 中国 湖南 锡矿山锑矿床 灰岩、黑色页岩、砂岩 Hu and Peng，2018 贵州 半坡锑矿床 石英砂岩、砂质泥岩、页岩 肖宪国，2014 云南 木利锑矿床 硅质岩、黑色页岩 韩江，2020 西藏 扎西康Sb-Pb-Zn矿床 灰黑色页岩、泥质和钙质页岩 Liang et al.，2018 澳大利亚 Victoria Costerfield Sb-Au矿床 富黄铁矿粉砂岩、炭质页岩 Wilson et al.，2017 New England Orogen Hillgrove锑矿床 页岩、石英砂岩、灰岩 Boyle and Hill，1988 加拿大 New Brunswick The Lake George锑矿床 砂岩、泥岩 Scratch et al.，1984 Newfoundland Beaver Brook锑矿床 黑色页岩、砂岩、砾岩 Lake and Wilton，2006 俄罗斯 The kolyvan-tomsk folded area Semiluzhinskoe Au-Sb矿床 炭质页岩、钙质页岩 Kalinin et al.，2015 美国 California McLaughlin锑矿床 泥岩、粉砂岩、灰岩、砾岩 Sherlock et al.，1995 吉尔吉斯斯坦 — Kadamzhai and Khaidarkan锑矿床 灰岩、灰绿色页岩、黑色页岩 Hnylko et al.，2019 — Atebayue锑矿床 砂岩、粉砂岩 Zhou et al.，2018 西班牙 SAN Antonio, Badajoz Alburquerqu锑矿床 角砾岩、钙质页岩组、硅质层 Gumiel and Vindel，1983 Ciudad Real San Felipe锑矿床 砂质页岩、石英岩 Ciudad Real Nazarena 锑矿床 砂质页岩、石英岩 葡萄牙 Braganca Braganca锑矿床 砾岩、石英岩、黑色板岩 Neiva et al.，2008 Porto Alto do Sobrido锑矿床 黑色泥页岩、砂岩、黑色泥质片岩 Simoes，1997 德国 Rhenish地块北部 Arnsberg锑矿床 富黄铁矿的黑色页岩和硅质灰岩 Wagner and Boyce，2003 
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表 2 国内外典型锑−金矿床Au-Sb品位
Table 2. Au–Sb ore grade of typical antimony gold deposits at home and abroad
国家 矿床名称 Au品位/×10−6 Sb品位/% 参考文献 中国 湘中沃溪Sb–Au–W矿床 8.1 3.50 陈明辉，2016 湘中龙山Au–Sb矿床 2.51~5.91 1.93~6.63 文琴和刘涛，2019 西藏马扎拉Au–Sb矿床 2~18.6 3.16~41.67 莫儒伟等，2013 西秦岭早子沟Au–Sb矿床 3.34 1.34 耿建珍等，2019 捷克 Krásná Hora Sb–Au矿床 3~5 1.5~3 Němec and Zachariáš，2018 俄罗斯 Sarylakh and Sentachan Au–Sb矿床 8~35 20~30 Bortnikov et al.，2010 俄罗斯 Semiluzhinskoe Au–Sb矿床 2 0.1~21 Kalinin et al.，2015 澳大利亚 Hillgrove Au–Sb 矿床 4~5 3~4 Ashley et al.，2000
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