Rb-Sr Dating of Sphalerites from Shizishan Pb-Zn Deposit in Huayuan Ore Concentration Area, Western Hunan, and Its Geological Significance
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摘要: 花垣矿集区位于扬子地块东南缘与雪峰(江南)造山带的过渡部位, 是湘西-鄂西成矿带的重要组成部分.狮子山铅锌矿床的发现是近年来湘西-鄂西成矿带矿地质勘查的重大进展之一, 该矿床位于矿集区中部, 主矿体呈层状、似层状展布, 与地层产状一致, 直接容矿围岩为下寒武统清虚洞组下段第三亚段藻灰岩, 矿体与围岩界线截然, 伴有方解石化等热液蚀变, 矿石矿物成分相对简单, 主要为闪锌矿, 少量方铅矿和黄铁矿.采用全溶方法和流体包裹体淋滤法对该矿床主成矿期的闪锌矿及其残渣进行Rb-Sr等时线法定年, 获得矿物相+残渣相的年龄为410±12 Ma(MSWD=2.20), 地质时代为早泥盆世, 明显晚于赋矿地层的时代.据此认为矿床的形成可能与加里东运动后构造伸展引起的盆地流体运移有关.该年龄对于整个花垣矿集区的铅锌成矿时代具有同样约束意义.闪锌矿+残渣的Sr初始值(87Sr/86Sr)i为0.709 16, 高于赋矿围岩, 与上覆寒武系白云岩地层的87Sr/86Sr值相近, 表明矿床形成时有来自上覆地层物质的加入.结果表明, 采用闪锌矿Rb-Sr等时线定年方法通过单矿物及其残渣相互约束, 可以有效确定成矿时代.Abstract: The Huayuan ore concentration area in the western Hunan Province, located in transitional zone between the southeastern margin of Yangtze block and the Xuefeng (Jiangnan) orogenic belt, is important section of the Xiangxi-Exi metallogenetic belt, and is the only one which occurs in limestone of Lower Cambrian strata in the Yangtze block. The Shizishan Pb-Zn deposit which was one of recently discovered Pb-Zn deposits in Xiangxi-Exi metallogenetic belt is located in the center of the Huayuan ore concentration area, and its main ore bodies occur in stratoid with the same trending as the strata and are sharply bounded by wall rocks with weak hydrothermal alteration such as calcitization. Ore bodies are strictly controlled by algal limestone of the third section of the lower member of the Lower Cambrian Qingxudong Formation. Ore minerals are mainly sphalerite, and a small amount of galena and pyrite, whereas gangue mineral is mainly calcite, and a small amount of barite and fluorite. Using the total-sample-dissolution method and leaching method to sphalerite in the Shizishan Pb-Zn deposit for Rb-Sr isochron dating. The isochron ages are obtained 410±12 Ma (MSWD=2.20) with initial 87Sr/86Sr value of 0.709 16 for mineral-phase+residue phase, which shows that the Early Devonian is the main time for the formation of the Shizishan Pb-Zn deposit. Research results indicate that the formation of the deposit is probably related to the regional migration of the basin fluid when the crust is stretched behind the Late Caledonian tectonic movement in Early Devonian, and the age is also a constraint on the Pb-Zn ore-forming time of the whole Huayuan ore concentration area. The initial 87Sr/86Sr value of the mineral phase+residue phase is 0.709 16, which is slightly higher than those of the ore-bearing limestone, and close to those of the overlying dolostone of Middle-Upper Cambrian strata, indicating that the ore-forming materials of the ore bodies in the Shizishan Pb-Zn deposit are possibly derived from the overlying dolostone strata. It is thus concluded that direct dating of the ages of metal minerals by using Rb-Sr isochron method for single minerals and mineral residues could serve as a routine dating method.
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湘西花垣矿集区位于扬子地块东南边缘与雪峰(江南)造山带的过渡部位,是湘西-鄂西成矿带的重要组成部分.自20世纪70年代先后探明李梅和渔塘铅锌矿床以来,花垣矿集区一直备受关注,近年来,在渔塘矿区外围的狮子山、花垣断裂北侧杨家寨以及李梅矿区东部大脑坡等地区先后发现了隐伏铅锌矿矿体,找矿工作取得重大突破.目前,区内已探明铅锌储量超过500万吨,估算铅锌资源量在1 500万吨以上,达超大型规模.许多学者对该区铅锌矿床地质特征、成矿流体性质和矿床成因做过大量研究,先后提出过多种成因认识,如热液卡斯特成因(刘宝珺和王剑,1990)、多因复成矿床(舒见闻和彭国忠,1986;夏新阶和舒见闻,1995)、沉积-改造矿床(李宗发,1991)、低温热卤水成因(彭国忠,1986)和MVT矿床(刘文均和郑荣才, 1999, 2000;杨绍祥和劳可通,2007)等.有学者认为该区铅锌矿床于早寒武世形成矿源层,在加里东末期和印支-燕山期受构造热液作用分别形成似层状矿体和脉状矿体,具有多期成矿的特点(舒见闻和彭国忠,1986;李宗发,1991;夏新阶和舒见闻,1995),也有学者认为矿床形成于加里东末期(彭国忠,1986;杨绍祥和劳可通,2007).目前,在花垣矿集区除了矿石铅同位素模式年龄(李宗发,1991),尚无确切的年代学资料,原因是对产于碳酸盐岩地层中的铅锌矿床成矿年龄的精确测定一直是世界性的难题(李文博等,2002),即便是全球研究程度最高的MVT矿床也是如此(Sangster,1996;Leach et al., 2001, 2005).成矿年代的不确定性造成对矿床成因认识上的差异,已严重制约着对本区成矿作用和区域成矿规律的系统认识,影响到找矿工作的部署.近年来,随着分析测试技术的改进和分析精度的提高,采用Rb-Sr等时线法直接对闪锌矿进行定年被证明是测定浅成低温热液硫化物矿床成矿年龄的有效方法(Nakai et al., 1990, 1993;Christensen and Halliday, 1995;Christensen et al., 1995;刘建明等,1998;李文博等,2002),并在国内获得不少成功的实例(李文博等,2004;李厚民等,2007;张长青等,2008;蔺志永等;2010;王晓虎等,2011;朱飞霖等,2011;杜国民等,2012;胡乔青等,2012;张家菁等,2012;徐贻赣等,2013).本文在详细研究狮子山铅锌矿床地质特征的基础上,对主成矿期闪锌矿进行Rb-Sr同位素定年研究,获得了精确的年龄数据,为厘定成矿时代和矿床成因提供了新的可靠证据.
1. 花垣矿集区地质背景
花垣铅矿集区位于扬子陆块东南缘与雪峰(江南)造山带的过渡区(杨绍祥和劳可通,2007),往南西方向延伸至贵州松桃嗅脑,直至铜仁卜口场等地.构造上该区位于NE向湘黔断裂带中部(刘文均,1985;杨志坚,1987),经历了晋宁期碰撞造山、加里东期拉张裂陷-被动大陆边缘盆地-前陆盆地(尹福光等,2001)以及印支期-燕山期陆内变形等演化过程,形成了多种沉积/层控金属矿产和非金属矿产.加里东期末发生的造山运动,使扬子陆块边缘斜坡带褶皱隆起形成江南古陆,并导致本区隆起遭受长期风化剥蚀(杜远生和徐亚军,2012),因而缺失中志留统-中泥盆统地层,印支-燕山运动使盖层普遍发生褶皱变形.
矿集区内出露南华系至奥陶系海相地层,其中以寒武系地层出露最广(图 1).南华系出露于矿集区西南部,下部板溪群为浅灰绿色粉砂质板岩、绢云母板岩,中部大塘坡组为黑色薄层状炭质泥岩夹菱锰矿层、灰岩透镜体,为重要含锰矿层位,南沱组为灰、深灰色厚层块状冰碛砾岩、含砾砂屑泥岩;震旦系陡山沱组为深灰色厚层状粉晶白云岩与黑色薄层状炭质泥岩不等厚互层,向上白云岩增多,灯影组为浅灰、灰色厚层状粉晶-细晶白云岩夹亮晶颗粒白云岩;寒武系出露齐全,自下而上分别为:下寒武统牛蹄塘组,为黑色薄层状含炭泥岩;石排组灰色薄-中厚层状粉砂质泥岩、粉砂岩夹岩屑细砂岩;清虚洞组下部为灰色中厚层状泥质灰岩、泥晶灰岩、藻灰岩,上部为浅灰、灰白色中厚层状白云质灰岩夹砂屑鲕粒灰岩;中统高台组为灰白色薄-中层状粉细晶白云岩;中-上寒武统娄山关组为浅灰、灰白色厚层块状粉细晶白云岩夹亮晶颗粒白云岩.奥陶系仅分布于矿集区西北角,主体由灰岩组成.第四系零星分布于沟谷中.
图 1 花垣矿集区地质矿产简图(据湖南省地质调查院吉首矿产地质调查所,湖南龙山-保靖铅锌矿评价成果报告, 2009, 修编)1.地层界线;2.断裂及编号;3.铅锌矿床;Nh1bx.南华系板溪群;Nh2d.南华系大塘坡组;Nh2n.南华系南沱组;Z.震旦系; 1n-s.下寒武统牛蹄塘组+石牌组;−C 1s.下寒武统石牌组;−C 1q.下寒武统清虚洞组;−C 2g/−C 2a/−C 2c.中寒武统高台组组/熬溪组/车夫组;−C 2-3l.中-上寒武统娄山关组;O.奥陶系;F1.张家界-花垣断裂;F2.麻栗场断裂;F3.松桃-水田断裂−C Fig. 1. Sketch map of geology and minerals of the Huayuan ore concentration area in western Hunan Province寒武系沉积由早到晚经历了浅水陆棚-碳酸盐缓坡-开阔台地-局限台地的碳酸盐台地生长过程,其中由缓坡向开阔台地演化的过程中,由于同沉积断裂的活动以及藻类的快速生长在区内形成了分布广泛的藻礁(丘)(汤朝阳等,2012);在湘黔交界长达120 km、宽20 km的区域内,铅锌矿均产于清虚洞组藻灰岩中,明显受层位和岩性控制,藻灰岩的厚度变化通常与矿化富集呈正相关关系,其厚度在100 m以上对成矿更有利(李宗发,1991;杨绍祥和劳可通,2007).至中寒武世晚期,同沉积断裂活动往东迁移至麻栗场一带,在麻栗场断裂东西两侧沉积环境发生明显分异,即断裂以东沉积了一套富含泥质的碳酸盐岩(车夫组和比条组),西部则为白云岩沉积(娄山关组).
区内未见岩浆岩出露;除板溪群发生轻微变质作用外,其余地层均未受到变质作用影响.
区内发育一系列北北东、北东向断裂,它们共同构成湘黔断裂带(刘文均,1985;杨志坚,1987),最主要的有张家界-花垣断裂(F1)、麻栗场断裂(F2)和松桃-水田断裂(F3),为早期控相、后期控矿的深大断裂,花垣铅锌多金属矿集区即局限于这3条断裂及其所控制的下寒武统清虚洞组藻灰岩中.
2. 狮子山矿床地质特征
狮子山铅锌矿床位于花垣矿集区中部(图 1),是地质大调查期间新发现的大型铅锌矿床.矿区内主要出露寒武系清虚洞组,其次为高台组和娄山关组(图 2).据岩性组合特征,清虚洞组可分为上、下两段.下段以灰岩为主,且具有由下往上钙质含量增加、泥质含量减少的特点,又可细分为4个亚段,其中第三亚段主体为灰、浅灰色厚层-块状藻礁灰岩,为铅锌矿的主要赋矿层位,第四亚段为浅灰色中厚层状、斑块状含白云质亮晶砂屑灰岩夹含藻砂屑灰岩、藻灰岩,为矿区次要容矿层位.
矿区地质构造以北东向的狮子山背斜为代表,轴部地层为清虚洞组,两翼为高台组和娄山关组.区内断裂构造发育,以北东向断裂为主,次为北北东、北西、近南北向断裂.其中与成矿关系密切的断裂为北东向和北北东向断裂(图 2).
铅锌矿体主要赋存于清虚洞组下段藻灰岩中,多为隐伏矿体,一般有4~7层.矿体形态简单,以整合似层状为主,脉状次之,区内共圈定46个矿体,其中似层状矿体32个(大于2万吨的矿体15个,最大矿体达15万吨),333+3341铅锌金属资源量94万吨.似层状矿体走向以北东为主,北北东向、近南北向及近东西向有少量矿体;倾向以北西为主,倾角一般5°~9°,局部因断裂构造影响,可变陡至15°~25°;矿体沿走向延伸长一般为800~3 000 m,倾向延伸100~350 m,矿体厚一般2.6~3.1 m,最厚9.73 m;矿石组分以Zn为主,Pb+Zn平均品位为3.57%,伴生有益组分Cd.脉状矿体与围岩高角度斜交,表明其形成时代较晚,暗示区内具有明显的两期成矿作用.脉状矿体走向北东,倾向以南东为主,倾角一般70°~80°.矿物组合简单,矿石矿物主要为闪锌矿,次为方铅矿、黄铁矿,脉石矿物主要为方解石,含少量重晶石和萤石.矿石构造主要为斑脉状和网脉状,其次为浸染状构造、块状构造、细脉状构造等.矿石结构以他形-半自形晶粒结构、充填或填隙结构为主,偶见胶状结构及压碎结构等.矿床围岩蚀变以方解石化为主,其次为重晶石化、沥青化、萤石化和褪色化等低温蚀变,褪色化现象分布普遍,但褪色边厚度多小于1 cm,表明交代作用弱.
3. 样品特征及分析结果
3.1 样品特征
本次用于Rb、Sr同位素定年的样品采自狮子山矿区8号坑道同一个似层状矿体,8件样品均为新鲜的斑脉状矿石,属主成矿阶段的产物,热液蚀变为方解石化(图 3a).闪锌矿呈细小斑块状和脉状产出,与藻灰接触面常见细粒黄铁矿分布(图 3b,3c).矿石矿物以闪锌矿为主,其次为黄铁矿,脉石矿物主要为方解石.闪锌矿为浅黄绿色,呈半自形-自形,大小一般为0.05~0.25 mm,以粒状集合体形式产于热液粗晶方解石与藻灰岩之间;闪锌矿晶体轮廓清晰(图 3d),未见矿物穿插、交代现象,其流体包裹体均一温度为120~170 ℃,为典型的低温热液矿物.
3.2 分析流程及分析结果
将样品破碎至80~100目,人工在双目镜下挑选不含可识别杂质的闪锌矿样品,纯度达98%以上,用稀酸和超纯水在超声波清洗皿中清洗干净,在室温下晾干备用.准确称取50~100 mg样品于聚四氟乙烯封闭溶样器中,加入适量85Rb+84Sr混合稀释剂和氢氟酸及高氯酸混合酸分解样品,采用AG50×8阳离子树脂交换技术分离和纯化Rb、Sr,其同位素质谱分析在MAT-261可调多接收质谱计上完成.整个同位素分析过程和仪器分别采用GBW04411、NBS607和NBS987标准物质进行监控.NBS987的87Sr/86Sr比值测定值为0.710 23±5(2σ),NBS607的Rb、Sr含量与87Sr/86Sr比值测定值分别为524.30、65.46、1.200 48±52(2σ),GBW04411的Rb、Sr含量与87Sr/86Sr比值分别为249.4±0.7、159.0±0.2和0.759 91±0.000 08(2σ),与其证书值在测定误差范围内完全一致,表明测试数据可信可靠.同位素分析样品制备的全过程均在净化实验室内完成,全流程Rb、Sr空白分别为1×10-10 g和2×10-10 g.本次样品测试在中国地质调查局武汉地质调查中心同位素实验室完成.
采用全溶方法和流体包裹体淋滤法对主成矿期闪锌矿(矿物相)及其残渣(残渣相,去除流体包裹后)和淋滤液(闪锌矿流体包裹体提取液)进行Rb、Sr同位素测定,分析方法和技术流程参见杜国民等(2012).等时线年龄计算采用Ludwig(2001)编写的ISOPLOT软件.衰变常数λ值为1.42×10-11 a-1,等时线回归计算时87Rb/86Sr比值采用3%误差,87Sr/86Sr比值采用0.03%误差.文中数据处理采用Geokit软件(路远发,2004).分析结果见表 1.
表 1 狮子山矿床闪锌矿Rb-Sr同位素分析结果Table Supplementary Table Rb-Sr dating data for sphalerites from the Shizishan Pb-Zn deposit样号 样品名称 Rb(10-6) Sr(10-6) 87Rb/86Sr 87Sr/86Sr 误差(±2σ) SZ-5 矿物相 0.394 2 8.868 0.128 2 0.709 87 0.000 10 SZ-6 0.341 5 26.400 0.037 3 0.709 33 0.000 09 SZ-7 0.084 4 26.590 0.009 2 0.709 15 0.000 04 SZ-8 0.358 5 14.640 0.070 6 0.709 54 0.000 02 SZ-9 0.260 7 7.324 0.102 6 0.709 70 0.000 12 SZ-12 0.131 7 8.331 0.045 6 0.709 42 0.000 03 SZ-13 0.261 8 10.280 0.073 4 0.709 55 0.000 10 SZ-5-1 0.508 7 10.080 0.145 5 0.709 96 0.000 30 SZ-5 残渣相 0.673 8 1.065 0 1.826 0 0.719 74 0.000 09 SZ-6 0.544 1 0.555 4 2.830 0 0.725 99 0.000 10 SZ-8 0.643 0 0.909 5 2.041 0 0.720 74 0.000 02 SZ-9 0.415 7 1.050 0 1.143 0 0.715 80 0.000 02 SZ-12 0.115 0 0.458 9 0.722 9 0.713 86 0.000 03 SZ-13 0.352 0 0.662 5 1.533 0 0.717 88 0.000 04 SZ-5 淋滤液 0.107 6 7.621 0.040 7 0.709 48 0.000 03 SZ-6 0.199 1 23.690 0.024 2 0.709 24 0.000 01 SZ-8 0.100 6 10.450 0.027 8 0.709 37 0.000 20 SZ-9 0.086 0 5.459 0.045 4 0.709 43 0.000 08 SZ-12 0.021 8 5.469 0.011 5 0.709 16 0.000 02 SZ-13 0.824 2 11.700 0.020 3 0.709 42 0.000 10 矿物相的Rb和Sr含量分别为0.084 4×10-6~0.508 7×10-6和7.324×10-6~26.590×10-6,变化范围比较大,Rb含量低,Rb/Sr比值为0.003~0.050,87Rb/86Sr值和87Sr/86Sr值分别为0.009 2~0.145 5和0.70915~0.7099 6.在图 4中,除样品SZ-12偏离等时线较远外,其余7个样品点分布合理,计算得到的等时线年龄为420±120 Ma(MSWD=0.03),Sr初始值(87Sr/86Sr)i为0.709 12,但由于Rb/Sr比值小,即Rb含量低,导致所得年龄误差较大.
据表 1,与矿物相和残渣相相比,淋滤液相的Rb含量明显降低,而Sr含量显著增大,但87Rb/86Sr值和87Sr/86Sr值较集中,说明Rb和Sr在闪锌矿的流体包裹体中的分异不明显,不能构筑成等时线.这是因为:原生包裹体溶液是直接从成矿母溶液中捕获的,其Rb/Sr比值与成矿母溶液一致,相互之间没有明显差别,在87Sr/86Sr-87Rb/86Sr图解上聚集在一个点上,不可能构筑成等时线(Nakai et al., 1993;Pettke and Diamond, 1995),所以包裹体溶液应该是设法去除的对象,不应该是等时线定年的主要测定对象(刘建明等,1998).
残渣相是指通过研磨淋滤去除流体后的闪锌矿,能满足Rb-Sr法定年的基本条件(Pettke and Diamond, 1995).狮子山矿床闪锌矿残渣相的Rb含量为0.115 0×10-6~0.673 8×10-6,明显高于矿物相和淋滤液,表明Rb主要赋存在闪锌矿残渣中;Sr含量则降低,为0.458 9×10-6~1.065 0×10-6;Rb/Sr比值为0.251~0.980;87Rb/86Sr和87Sr/86Sr比值有较宽的变化范围,分别在0.7229~2.8300和0.713 86~0.725 99之间.在图 5中,6个残渣相样品点具有良好的线性关系,计算得到的年龄为401±41 Ma(MSWD=3.6),(87Sr/86Sr)i值为0.709 40.
残渣相及与对应的矿物相共12个样品点在87Rb/86Sr-87Sr/86Sr图上具有良好的直线线性关系(图 6),计算得到的等线年龄为410±12 Ma(MSWD=2.2),(87Sr/86Sr)i值为0.709 16.误差明显减小,精度优于矿物相和残渣相所得数据,该年龄可作为矿床形成年龄,地质时代为早泥盆世.
4. 讨论
4.1 成矿年龄的可靠性
热液矿物Rb-Sr等时线测年的基本前提是同源、同时、封闭性、一致的(87Sr/86Sr)i以及具有不同的Rb/Sr(李文博等,2002).本次工作用于测试的样品采自同一矿体局部较小的范围内,为结晶较好的斑脉状矿石,闪锌矿纯度高,且与围岩界线区别明显,无后期矿物穿插、交代现象;样品点位不同保证其具有不同的Rb/Sr比值,能满足Rb-Sr同位素测年的前提条件.此外,在图 7中,1/Sr与87Sr/86Sr、1/Rb与87Rb/86Sr之间不存在线性关系,而且相对稳定,说明闪锌矿生长期间(87Sr/86Sr)i值基本上保持不变(Pettke and Diamond, 1996;李文博等,2002).因此,图 6所给出的直线具有等时线意义,可代表矿床的形成年龄.从野外地质现象也可得到佐证,如闪锌矿化沿热液方解石脉壁分布或产于方解石脉中,围岩中未见闪锌矿(彭国忠,1986);普遍见有闪锌矿沿顺层缝合线分布,均未穿过岩层层面,也表明矿化作用发生在深埋压溶环境,为后生热液成因.
研究表明,雪峰山地区在略早于419 Ma时经历了一次明显的构造热事件(胡召齐等,2010),而且,向西波及的界线可能为张家界-花垣断裂带(杜远生和徐亚军,2012).狮子山铅锌矿床的形成年龄为410±12 Ma,可能与这次构造热液事件有一定关系,构造热事件导致成矿流体向有利成矿部位汇集,最终形成矿床.
4.2 成矿物质来源
Sr同位素初始值(87Sr/86Sr)i是示踪成矿物质和成矿流体来源的有效途径之一(Bell et al., 1989).寒武纪海水和海相碳酸盐岩87Sr/86Sr值约为0.709 0(Denison et al., 1998),扬子陆块下寒武统水井沱组碳酸盐岩沉积时古海水87Sr/86Sr值为0.708 78(张自超,1995),重庆秀山地区寒武系下统灰岩87Sr/86Sr值为0.708 837,中-上统白云岩87Sr/86Sr值为0.709 175(黄思静等,2002).狮子山闪锌矿Rb-Sr等时线年龄给出的(87Sr/86Sr)i值为0.709 12~0.709 40(平均为0.709 23),高于寒武纪海水和海相碳酸盐岩的锶同位素比值,也高于扬子陆块和秀山地区下寒武统灰岩的相应比值,而与寒武系中-上统白云岩的比值较为接近,暗示闪锌矿沉淀结晶时有来自上覆地层物质的加入,与硫同位素的分析结果一致(李宗发,1992).
4.3 地质意义
狮子山铅锌矿床是花垣矿集区中新发现的一个大型铅锌矿,其成矿特征与矿集区内其他铅锌矿床(如李梅、渔塘、嗅脑等)具有相似性,如赋矿地层和围岩岩性一致,矿体产出特征相似,均产于清虚洞组藻灰岩中,矿石矿物均以闪锌矿为主,矿石结构构造相似,围岩蚀变特征相似,以方解石化为主.因此,本次获得的狮子山铅锌矿床的成矿年龄对于整个花垣矿集区的铅锌成矿时代具有同样的约束意义.此外,厘定的成矿作用发生于早泥盆世,与黔东南地区金矿成矿时代(朱笑青等,2006)和雪峰地区大部分金矿成矿时代(彭建堂和戴塔根,1998;王秀璋等,2000)基本一致,表明花垣至雪峰山地区普遍存在晚加里东期低温热液成矿作用.这次成矿作用可能与加里东运动后的伸展断陷作用引起的盆地流体大规模运移有关;这对于今后在花垣矿集区及邻区的找矿方向具有一定理论指导意义,即加里东晚期形成的地质构造及热液活动产物在找矿工作部署中是不可忽视的因素.
5. 结论
湘西花垣矿集区狮子山铅锌矿床主成矿阶段闪锌矿Rb-Sr同位素等时线年龄为410±12 Ma,表明矿床形成于早泥盆世,该年龄对于整个花垣矿集区的铅锌成矿时代具有同样约束意义.闪锌矿的(87Sr/86Sr)i值为0.709 12~0.709 40,高于赋矿围岩,而与上覆白云岩地层的87Sr/86Sr值相近,指示部分成矿物质可能来源于上覆地层;狮子山铅锌矿床是在加里东运动后构造伸展作用引起的大规模盆地流体活动的产物.
致谢: 野外工作期间得到了湖南省地质调查院405地质队刘健清队长、余沛然总工、张劲松工程师的大力支持,武汉地质调查中心同位素实验室蔡红高级工程师帮助测试样品,李华芹研究员对样品处理和分析测试过程给予了悉心指导,两位审稿专家提出了宝贵意见,在此一并致以诚挚的谢意. -
图 1 花垣矿集区地质矿产简图(据湖南省地质调查院吉首矿产地质调查所,湖南龙山-保靖铅锌矿评价成果报告, 2009, 修编)
1.地层界线;2.断裂及编号;3.铅锌矿床;Nh1bx.南华系板溪群;Nh2d.南华系大塘坡组;Nh2n.南华系南沱组;Z.震旦系; −C1n-s.下寒武统牛蹄塘组+石牌组; −C1s.下寒武统石牌组; −C1q.下寒武统清虚洞组; −C2g/ −C2a/ −C2c.中寒武统高台组组/熬溪组/车夫组; −C2-3l.中-上寒武统娄山关组;O.奥陶系;F1.张家界-花垣断裂;F2.麻栗场断裂;F3.松桃-水田断裂
Fig. 1. Sketch map of geology and minerals of the Huayuan ore concentration area in western Hunan Province
表 1 狮子山矿床闪锌矿Rb-Sr同位素分析结果
Table 1. Rb-Sr dating data for sphalerites from the Shizishan Pb-Zn deposit
样号 样品名称 Rb(10-6) Sr(10-6) 87Rb/86Sr 87Sr/86Sr 误差(±2σ) SZ-5 矿物相 0.394 2 8.868 0.128 2 0.709 87 0.000 10 SZ-6 0.341 5 26.400 0.037 3 0.709 33 0.000 09 SZ-7 0.084 4 26.590 0.009 2 0.709 15 0.000 04 SZ-8 0.358 5 14.640 0.070 6 0.709 54 0.000 02 SZ-9 0.260 7 7.324 0.102 6 0.709 70 0.000 12 SZ-12 0.131 7 8.331 0.045 6 0.709 42 0.000 03 SZ-13 0.261 8 10.280 0.073 4 0.709 55 0.000 10 SZ-5-1 0.508 7 10.080 0.145 5 0.709 96 0.000 30 SZ-5 残渣相 0.673 8 1.065 0 1.826 0 0.719 74 0.000 09 SZ-6 0.544 1 0.555 4 2.830 0 0.725 99 0.000 10 SZ-8 0.643 0 0.909 5 2.041 0 0.720 74 0.000 02 SZ-9 0.415 7 1.050 0 1.143 0 0.715 80 0.000 02 SZ-12 0.115 0 0.458 9 0.722 9 0.713 86 0.000 03 SZ-13 0.352 0 0.662 5 1.533 0 0.717 88 0.000 04 SZ-5 淋滤液 0.107 6 7.621 0.040 7 0.709 48 0.000 03 SZ-6 0.199 1 23.690 0.024 2 0.709 24 0.000 01 SZ-8 0.100 6 10.450 0.027 8 0.709 37 0.000 20 SZ-9 0.086 0 5.459 0.045 4 0.709 43 0.000 08 SZ-12 0.021 8 5.469 0.011 5 0.709 16 0.000 02 SZ-13 0.824 2 11.700 0.020 3 0.709 42 0.000 10 -
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