(1 成都理工大学沉积地质研究院, 四川 成都610059; 2 成都理工大学油气藏地质及 开发工程国家重点实验室, 四川 成都610059; 3 中国地质科学院矿产资源研究所, 北京100037; 4 成都理工大学地球科学学院, 四川 成都610059)
第一作者简介李启来, 男, 1989年生, 博士研究生, 沉积学专业。 Email: 6736558 92@qq.com
** 通讯作者伊海生, 男, 1959年生, 教授, 博士生导师, 主要从事沉积地质学研究 。 Email: yhs@cdut.edu.cn
收稿日期2016-03_08
本文得到国家科技支撑计划专题项目(编号: 2011BAB04B10_2)资助
of Beisi Formation in Dongping area, Guangxi, and its genetic study
(1 Institute of Sedimentary Geology, Chengdu University of Technology, Chengdu 610059, Sichuan, China; 2 State Key Laboratory of Oil/Gas Reservoir Geology and Exploration, Chengdu University of Technology, Chengdu 610059, Sichuan, China; 3 Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China; 4 College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, Sichuan, China)
2016-03_08
图 1广西含锰地层分区示意图(据茹廷锵等,1992修改) 1—国界线; 2—海岸线; 3—岛屿; 4—省界线; 5—含锰地层分区界线; 6—地名; 7 —研究区位置 Fig. 1Sketch map showing regionalization of manganese_bearing sequences in Gua ngxi (modified after Ru et al.,1992) 1—National boundaries; 2—Coastline; 3—Island; 4—Provintial boundary; 5—Dist rict boundaries of manganese_bearing Sequence; 6—Administrative place name; 7 —Location of the study area |
图 2东平锰矿区综合地层柱状图(据杜树三等,1994修改) 1—泥岩; 2—砂岩; 3—页岩; 4—灰岩; 5—竹叶状灰岩; 6—角砾状灰岩; 7—泥质 灰岩; 8—含锰泥质灰岩; 9—锰矿层; 10—钙质泥岩; 11—凝灰岩; 12—钙质砂岩 Fig. 2Comprehensive stratigraphic column of manganese_bearing rock assemblages in Dongping area(modified after Du et al.,1994) 1—Mudstone; 2—Sandstone; 3—Shale; 4—Limestone; 5—Edgewise conglomerate; 6— Brecciated limestone; 7—Argillaceous limestone; 8—Manganese_bearing argillac eous limestone; 9—Manganese mineralization beds; 10—Calcareous mudstone; 11—T uff; |
微量元素中,w(Sr)最高,平均为822.13×10-6,其次是w(Ba),平均为277.85×10-6,Zn、Rb、Zr、V平均质量分数介于50.00 ×10-6~100.00×10-6,Ni、Cr、Cu、Ga、Pb、Co、Li、Y质量分数介于10. 00×10-6~50.00×10-6,Sc、Th、Nb、Cs、W、U、Hf、Sb、Be、Mo质量分数 介于1.00×10-6~10.00×10-6,余下的Tl、Bi、Cd含量低,质量分数均小 于0.50×10-6。与世界大 洋热水铁锰结壳均值(Anikeeva et al.,2002)相比,Ba、Zn、Zr、V、Ni、Cu、Pb、Co 、 Li、Y、Nb、W、U、Hf、Sb、Mo、Tl、Bi、Cd等元素含量最大值均低于世界大洋热水铁锰结 壳均值,Sr、Sc、Th、Cs、Be等元素含量均值与之相当,而Rb、Ga等元素含量均值较高,Cr 含量较低(图3)。
表 1东平地区北泗组碳酸锰矿床元素含量数据 Table 1Element content of manganese carbonate deposits of the Beisi Formation in Dongping area |
图 3东平地区北泗组碳酸锰矿床和世界大洋热水铁锰结壳(Anikeeva et al.,2002)元 素含量分布图 Fig. 3Distribution of element content of manganese carbonate deposits of the B eisi Formation in Dongping area and hydrothermal crusts of the Worlds oceans (after Anikeeva et al.,2002) |
另外,样品Co/Ni比值均小于0.89,而 Co/Ni比值小于1是热水沉积的标志(杨瑞东等,2010)。 分析表明,东平地区北泗组碳酸锰矿床为热水沉积。
图 4东平地区北泗组碳酸锰矿床Fe_Mn_(Ni+Co+Cu) ×10三角图解(底图据Crerar et al.,1982修改) Fig. 4Triangular diagram of Fe_Mn_(Ni+Co+Cu)×10 for manganese carbonate depos its of the Beisi Formation in Dongping area(base map modified after Cre rar et al., 1982) |
图 5东平地区北泗组碳酸锰矿床Co/Zn_(Co+Ni+Cu) 相关图(底图据Toth,1980修 改) Fig. 5Correlation diagram of Co/Zn_(Co+Ni+Cu) for manganese carbonate deposits of the Beisi Formation in Dong_ ping area(base map modified after Toth ,1980) |
目前,国内锰矿床中有关Ga含量的数据主要有:贵州从江高增大塘坡组锰矿床中块状锰矿、 氧化锰矿、纹层状锰矿和含锰泥岩,w(Ga)平均值分别为18.70×10-6、15.90 ×10-6、6.56 ×10-6、18.80×10-6 (杨瑞东等,2010)(图6:7、10~12);贵州水城茅口组锰矿床中w( Ga)介于3.77×10-6~80.30×10-6,平均值为13.87×10-6,其中 锰矿层和围岩w(Ga)平均值分别为14.92×10-6和10.93×10-6 (杨瑞东等,2009)(图6:8、9);贵州遵义锰矿 白泥塘层硅质岩中w(Ga)介于0.23×10-6~11.10×10-6之间,平 均值为3.31×10-6(刘志 臣等,2013)(图6:5);广西下雷地区五指山组锰矿床中w(Ga)介于1.71×1 0-6~56.40×10-6, 平均值为15.56×10-6, 其中锰矿层和围岩w(Ga)平均值分别为22.96×10-6、5.69×10-6(张超,2013) (图6:6、13);贵州松桃杨家湾锰矿层中w(Ga)平均值为40.27×10 -6 (何志威等,2013)(图6:14)。与这些资料相比(图6),北泗组碳酸锰矿床围岩中Ga含 量高于国内大部分锰矿层中Ga含量,而锰矿层中Ga含量相对为最高。
图 6沉积岩(Anikeeva et al.,2002;陈骏等,2004)、国内锰矿床(杨瑞东等,2009 ;2 010;刘志臣等,2013;张超,2013;何志威等,2013)、国外锰矿床(Sugisaki et al., 1991;Kazachenko et al.,2006;Mishra et al.,2006)、富Ga矿层(Fechner,1985;Z hao et al.,2009;王行军等,2015)及东平地区北泗组碳酸锰矿床中Ga含量分布 图 Ⅰ—沉积岩或矿层; Ⅱ—围岩; Ⅲ—东平地区北泗组碳酸锰矿Ga含量均值等值线; Ⅳ— 数据分类界线 Fig. 6Distribution of content of Ga in sedimentary rock (after Anikeeva et al. , 2002; Chen et al., 2004), manganese ore deposits in China (after Yang et al., 2 009; 2010; Liu et al., 2013; Zhang, 2013; He et al., 2013) and abroad (after Sug isaki et al., 1991; Kazachenko et al., 2006; Mishra et al., 2006), gallium_rich ore beds (after Fechner , 1985; Zhao et al., 2009; Wang et al., 2015) an d mangan ese carbonate deposits of the Beisi Formation in Dongping area Ⅰ—Sedimentary rock or ore bed; Ⅱ—Surrounding rock; Ⅲ—Contour lines of the average content of Ga in manganese carbonate deposits of the Beisi Formation i n Dongping area; Ⅳ—Classification boundaries of data |
迄今为止,尚无发现Ga的独立矿床(Zhao et al.,2009),Ga主要产于铝土矿、闪锌矿和 煤矿之中(Christie et al.,2002;Zhao et al.,2009;Sverdrup et al.,2014)。部 分铝土矿、闪锌矿和煤矿矿层中Ga含量与北泗组碳酸锰矿床矿层中Ga含量相当,甚至比之小 (图6)。例如,产有超大型Ga矿床的内蒙古准格尔煤田黑岱沟矿区6煤矿,其w(Ga)平 均值 为44.80×10-6(Zhao et al.,2009)(图6:25);美国阿拉斯加闪锌矿和铝土矿 中w(Ga) 平均值皆为50.00×10-6(Fechner ,1985)(图6:26、27);滇东南地区铝土矿 中w(Ga) 平均值为28.86×10-6(王行军等,2015)(图6:24)。铝土矿、闪锌矿和煤矿中G a的最低 工业品位w(Ga)分别为20.00×10-6、100.00×10-6和30.00×10-6 (邵厥年等,2010),但 目前,尚无锰矿中Ga的最低工业品位要求。参照煤中Ga的工业品位要求,则15件北泗组碳酸 锰矿床样品中,有8件样品的w(Ga)>30.00×10-6,占53.33%,其中锰矿层和围 岩样品中分别 有75.00%和28.57%的样品Ga含量达到工业品位要求。因此,以Ga含量来看,东平地区北泗 组碳酸锰矿床具有成为Ga矿床的可能,但其商业价值有待进一步研究。
此外,东平地区北泗组碳酸锰矿床上覆百逢组底部地层w(Ga)平均值为12.73×10- 6,下伏马 脚岭组顶部地层w(Ga)平均值为12.64×10-6(伊海生等,2015),明显低于北 泗组锰矿床中 的w(Ga)平均值33.76×10-6。因此,在区域上,高含量的Ga可以作为寻找类似 东平碳酸锰矿床的一个地球化学标志。
与上述铁锰沉积不同,东平地区北泗组碳酸锰矿床中Ga与Al的相关系数仅为0.28,与Mn的 相 关系数却高达0.99(图7a、b)。最近,在白令海中也有类似的发现。白令海热水铁锰结壳 中G a平均含量为37.59×10-6,Ga与Al的相关系数为-0.68,与Mn的相关系数高达0.98 (Baturin et al.,2010)。关于Ga在这类铁锰结壳中的赋存情况,有学者进行了初步研究。Koschins ky等(2003)首先研究了亚热带西太平洋和大西洋水成和热水铁锰结壳,发现水成和热液铁 锰结壳中分别有90.47%和95.85%的Ga赋存在锰氧化物之中,二者w(Ga)平均值分别为1 9.10× 10-6、12.87×10-6。Mikhailik等(2015)研究了日本海Belyaevsky海底山 热水铁锰结壳, 结果显示79.40%的Ga赋存在锰氧化物之中,w(Ga)平均值为19.10×10-6。由此 看来,东平地区北泗组碳酸锰矿床中Ga的赋存与含锰矿物密切相关。
图 7古代锰矿床(杨瑞东等,2009;本研究)和现代大洋铁锰沉积(Dubinin et al.,20 06;2008;Anikeeva et al.,2008; Baturin et al.,2010;2012) Al_Ga(a)、Mn_Ga (b)交会图 图中虚线为Ga的克拉克值19.00×10-6(Dubinin et al.,2008) Fig. 7Cross plots of Al_Ga(a) and Mn_Ga(b) for manganese ore deposits (after Yang et al.,2009;this study) and ferromanganese deposits form the ocean (after Dubi nin et al.,2006;2008;Anikeeva et al.,2008;Baturin et al.,2010;2012) The dotted line in the diagram shows the clark value of Ga, 19.00×10-6 ( after Dubinin et al.,2008) |
Zn/Co比值是判别沉积环境最为有效的指标之一(Sugisaki et al.,1991),东平地区北泗 组碳 酸锰矿床样品Zn/Co平均值为4.69,与边缘海(日本海)铁锰沉积物中Zn/Co值(Kinoshita et al.,1981)相当。Mikhailik等(2015)认为日本海Belyaevsky海底山铁锰结壳中Ga主要来 源于富Ga的长白山火山灰,而北泗组凝灰岩中w(Ga)平均值为16.50×10-6 (伊海生等,2015 ),与正常火成岩均值(刘英俊等,1984)相当,异常不明显,而与北泗组碳酸锰矿床中 w(Ga)平均值33.76×10-6相差较大。另外,因构造、岩浆热液、风化淋滤和地下 水活动等作用 富集形成的Ga常与Al呈较好的正相关性(翟秀静等,2010;陈阳等,2013;张勇等,2014) ,而北泗组碳酸锰矿床中Ga与Al相关性差,相关系数为0.28。这意味着东平地区北泗组碳 酸锰矿床中Ga来源于凝灰岩的可能性不大。
海底热液活动产物包括热液流体、热液硫化物、喷口生物、热液柱、热液蚀变岩石、含金属 沉积物和自然元素等(曾志刚,2011)。目前已有的诸多报道(Krupp et al.,1987;1990 ; Glasby et al.,1997;Benézéth et al.,1997;Metz et al.,2000;Baturin et al. ,2011)显示,海底热液流体富含Ga。同时,海底热液硫化物中也有高含量Ga的报道(Iiza sa et al.,1999;Lein et al.,2003;Noguchi et al.,2007)。例如,在冲绳海槽和菲 律宾海Suiyo海底山热液硫化物中,w(Ga)分别高达3700.00×10-6和1440. 00×10 -6(Noguchi et al.,2007)。另外,Bull(1991)和Colwell(1997)认为海洋生物亦能够富集Ga。据东 平地区锰矿钻孔资料分析,北泗组地层及矿层厚度呈带状延伸,明显受线性构造控制,反映 出北泗组碳酸锰矿床沿同生断裂带展布,沉积时期海底热液活动活跃(杜树三等,1994;李 升福等,2009;伊海生等,2015;谢华,2015)。同时,有机地球化学分析也表明北泗组碳 酸锰矿床中有机质主要来源于热液喷口微生物群落(伊海生等,2015)。据此推断,东平地 区北泗组碳酸锰矿床中Ga的来源与海底热液活动有关。
图 8现代大洋铁锰沉积(Anikeeva et al.,2008;Dubinin et al.,2008;Baturin et al.,2010;2012)及古代锰矿床(张超,2013; 本研究)Mn/Fe_Ga(a)、Co_Ga(b)对 数坐标交会图 红色—现代大洋热水铁锰沉积; 蓝色—现代大洋水成铁锰沉积; 黑色—古代锰矿床 Fig. 8Logarithmic coordinate cross plot of Mn/Fe_Ga (a) and Co_Ga (b) for ferr omanganese deposits form the ocean (after Anikeeva et al., 2008; Dubinin et al ., 2008; Baturin et al., 2010; 2012) and manganese ore deposits (after Zhang, 2013; this study) Red—Hydrothermal ferromanganese deposits form the ocean; Blue—Hydrogenic ferro manganese deposits form the ocean; Black—Manganese ore deposit |
(2) 东平地区北泗组碳酸锰矿床地球化学特征显示,相对于世界大洋热水铁锰结壳元素含 量均值,其明显富集Rb、Ga等元素,Al、K、Sr、Sc、Th、Cs、Be等元素含量均值与之相当 ;Fe_Mn_(Ni+Co+Cu)×10三角图解、Co/Zn_(Co+Ni+Cu)相关图以及Co/Ni值表明北泗组碳酸 锰矿床为热水沉积。
(3) 通常,Ga与铝硅酸盐关系密切,而东平地区下三叠统北泗组碳酸锰矿床中Ga与Al的相 关系数仅为0.28,与Mn的相关系数高达0.99。结合现代大洋铁锰沉积有关Ga的最新报道, 研究表明北泗组碳酸锰矿床中Ga的赋存与含锰矿物密切相关,来源与海底热液活动有关。
(4) 利用Mn/Fe_Ga、Co_Ga的关系图可判别古代铁锰沉积的成因类型。
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