Genesis and tectonic setting of the Dongqiao peridotites in the central segment of the Bangong Co-Nujiang Suture Zone
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摘要:
东巧蛇绿岩位于班公湖—怒江缝合带中段，根据地理位置特征并以强玛镇为中心将东巧岩体划分为东西两个岩体。其中西岩体相对面积较大，由地幔橄榄岩、枕状玄武岩、辉长辉绿岩等组成；而东岩体面积较小，仅含地幔橄榄岩部分，各个不同单元之间呈断层接触关系。对东巧地幔橄榄岩开展岩石学、矿物学及地球化学研究发现：(1)东巧地幔橄榄岩以方辉橄榄岩为主，纯橄岩所占比例较小，约15%。豆荚状铬铁矿主要呈条带浸染状赋存在厚层且延伸较远的纯橄岩中。(2)东巧地幔橄榄岩中单斜辉石含量小于3%，矿物地球化学和全岩地球化学特征显示其来源于尖晶石相地幔源区的部分熔融，且部分熔融程度较高，估算在22%~28%，高于深海地幔橄榄岩的部分熔融程度(10%~22%)。(3)东巧地幔橄榄岩中的副矿物铬尖晶石Cr#值较高大于60，全岩具有U型球粒陨石标准化稀土元素配分模式，同时Rb、U、Zr和Sr相对富集，Hf和Nb相对亏损。全岩的地球化学特征指示了俯冲带之上的残余地幔与流体/熔体发生了反应，致使轻稀土元素以及部分微量元素选择性富集。综合东巧地幔橄榄岩的矿物化学组成成分以及全岩的地球化学特征，认为东巧地幔橄榄岩形成于大洋中脊的扩张环境中，后受到洋内俯冲作用的影响，导致俯冲带之上高度部分熔融的地幔橄榄岩与流体/熔体发生相互作用。
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关键词:
- 地幔橄榄岩 /
- 部分熔融 /
- 流体/熔体-岩石反应 /
- 东巧蛇绿岩 /
- 班公湖-怒江缝合带
Abstract:Located in the central segment of the Bangong Co-Nujiang Suture Zone, the Dongqiao ophiolite is divided into east and west massifs. The research on the origin and tectonic setting of the ophiolite in the Bangong Co-Nujiang suture zone can provide key clues for revealing the tectonic evolution of the Neo-Tethys and the collision between the Indian plate and the Eurasian plate. The area of the west rock massif is relatively large, consisting of mantle peridotites, pillow-like basalts, gabbros, diabases, etc., while the area of the east massif is small and contains only part of mantle peridotites, with the faults being in contact between different units. Based on petrology, mineralogy and geochemistry of the peridotites in Dongqiao ophiolite, the authors have reached some conclusions:(1) The Dongqiao peridotites are dominated by harzburgites, with minor proportion of dunites (about 15%). The podiform chromitites mainly show banded and disseminated structures, and occur in a thick layer of far-extending dunites. (2) The clinopyroxene content of Dongqiao peridotites is less than 3%. The mineral and the whole-rock geochemistry show that Dongqiao peridotites were formed after 22%-28% degree of partial melting of the spinel-phase mantle source, higher than the partial melting of abyssal peridotites (10%-22%). (3) The Cr# values of spinels in the Dongqiao peridotites are higher than 60. The chondritenormalized REE patterns of the Dongqiao peridotites display enrichments in LREE. In the primitive mantle-normalized spider diagrams, the Dongqiao peridotites exhibit slightly positive Rb, U, Zr, Sr anomalies and slightly negative Hf, Nb anomalies. These geochemical characteristics jointly indicate the selective enrichments of LREE and some trace elements according to interaction between the residual mantle and the fluid/melt above the subduction zone. Based on the mineral composition and the whole-rock geochemical characteristics of Dongqiao peridotites, the authors hold that the Dongqiao peridotites were formed in the dilated environment of the mid-ocean ridge, and then were influenced by intra-ocean subduction, resulting in highly partially melted peridotites interacting with the fluid/melt above the suprasubduction zone.
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1. 研究目的（Objective）
甘肃省高台县大青山地区地处阿拉善地块龙首山基底杂岩带，位于酒东盆地马营凹陷东段山前沉积盆地北缘（图 1a）。区内主要出露有古元古界—新太古界龙首山岩群、中元古界蓟县系墩子沟群、海西期侵入岩、侏罗系龙凤山组和白垩系庙沟组（图 1b）。
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图 1 甘肃省高台县大青山地区大地构造位置图（a）、区域地质图（b）以及ZK1201岩性柱状图（c），含油气岩心照片（d-g）和油气成藏模式图（h）Figure 1. Tectonic location (a), regional geological map(b), lithology column(c) and drill photos of ZK1201 (d-g), hydrocarbon accumulation pattern (h) in the Daqingshan area of Gaotai County, Gansu Province为实现研究区金属资源和油气资源的综合调查，中国地质调查局发展研究中心联合甘肃省地调院、探矿工程所、吉林大学在前期“甘肃省高台县臭泥墩—西小口子地区三幅1∶5万矿产远景调查”项目基础上，通过开展专题地质填图、矿产综合信息预测、智能找矿预测等工作，部署实施钻孔ZK1201，以期实现找矿突破。
2. 研究方法（Methods）
利用研究区地质调查、磁法、激电测深、化探数据和无人机影像等资料，开展综合信息解译。采用卷积和孪生网络神经网络模型对区内典型金属矿床成矿作用特征标志、油气赋矿层位进行深度学习，提出工程验证建议。钻探验证所采用钻机为汽车钻，整机包括车底盘、动力系统、液压系统、操控系统等。
3. 结果（Results）
在综合研究和智能预测的基础上，布设的ZK1201孔在钻穿早二叠世花岗闪长岩（图 1c）后，钻遇地层，续钻至393.8 m后终孔（图 1c）。此次工作共钻遇中侏罗统龙凤山组地层220 m，共发现14层油层（总厚145 m，单层最大厚度28 m，最小厚度1.4 m）。钻孔含油性由上部砾岩（油斑级以下）向下部砂岩（富含油或饱含油）逐渐增多，其中高角度裂缝普遍见可流动原油（图 1d~g）。经国家地质实验测试中心分析，原油中饱和烃、芳烃含量分别占32.4%和34.6%，为高品质轻质原油。原油中正构烷烃分布完整，主峰碳数、奇偶优势及甾烷和藿烷分布都指示其陆相烃源岩来源。
野外地质调查发现，白垩系庙沟组近水平发育，与下伏侏罗系龙凤山组呈角度不整合接触。庙沟组主要由厚层暗色泥岩组成，并发育薄层暗色粉砂质泥岩，可能为区域烃源岩层。初步判断成熟的烃源岩排出的油气沿角度不整合运移至侏罗系砂砾岩和砂岩储层后，被逆冲推覆花岗岩体封闭，形成构造-岩性油气藏（图 1h）。
研究发现区域内沉积盆地最南缘边界处在祁连山北缘断裂之下，最北缘处在龙首山断裂的下盘，南北跨度约80 km。区域内沉积地层较厚，其中侏罗系龙凤山组厚约2100 m，白垩系庙沟组厚约900 m，说明研究区具有较大的成藏潜力。此次油气藏的发现，预示着大青山地区具有完整的油气成藏系统，显示出良好油气勘探前景。建议进一步加强油气基础地质调查研究工作。
4. 结论（Conclusions）
（1）在大青山地区花岗岩逆冲推覆体之下的中生代沉积地层中发现原油，所发现的高品质轻质原油，具陆相烃源岩来源特征。
（2）研究区具有良好的油气勘探前景，建议进一步加强油气地质调查研究工作。
5. 致谢（Acknowledgement）
感谢甘肃省地质调查院董国强，北京探矿工程研究所渠洪杰、谭春亮以及国家实验测试中心沈斌在野外工作和样品测试过程中的协助。
致谢: 感谢西藏矿业公司教授级高工巴登珠的指导，野外期间还受到西藏自治区地质矿产勘查开发局第五地质大队董玉杰、张智霖、赤列、晁增华等人的帮助，电子探针测试在东华理工大学核资源与环境教育部重点实验室郭国林教授的帮助下完成，论文撰写过程中与邱添、卢雨潇、杨胜标等人进行了有益的讨论，审稿专家对本文提出了宝贵的修改意见，在此致以诚挚的谢意！ -
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图 1 西藏班公湖—怒江缝合带蛇绿岩分布简图(据Liu et al., 2016)
Figure 1. Geological sketch map of the Tibetan Plateau showing basic tectonic framework and the distribution of Bangong Co-Nujiang Suture Zone ophiolites (after Liu et al., 2016)
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图 2 班公湖—怒江缝合带中段东巧蛇绿岩地质简图(据西藏自治区地质矿产勘查开发局第五地质大队，2016❶简化)
Figure 2. Simplified geological map of the Dongqiao ophiolite in the central part of Bangong Co-Nujiang Suture Zone
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图 3 东巧蛇绿岩中不同的地幔橄榄岩类型以及铬铁矿矿体产出特征
a—方辉橄榄岩; b—方辉橄榄岩中的斜方辉石颗粒凸起; c—纯橄岩与方辉橄榄岩接触边界的矿体; d—纯橄岩与方辉橄榄岩接触部位的构造破碎带; e—茶绿色的蚀变纯橄岩; f—表面光滑的纯橄岩; g—纯橄岩中的矿石角砾; h—铬铁矿条带
Figure 3. Outcrops of the Dongqaio ophiolite and podiform chromitite in the central part of Bangong Co-Nujiang Suture Zone
a-Harzburgites; b-Protuberant pyroxenes on the harzburgites; c-The chromitite between dunites and harzburgites; d-The structural fracture zone between dunites and harzburgites; e-Strongly serpentinized dunites; f-Dunites with slick surface; g-Chromitite hosted by dunites; h-Chromitite band
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图 4 东巧地幔橄榄岩显微照片及背散射图像(图j~l)
a—方辉橄榄岩中破碎的橄榄石嵌入到斜方辉石粒间; b—方辉橄榄岩中橄榄石呈浑圆状包裹在斜方辉石中; c—方辉橄榄岩中斜方辉石边部呈港湾状与铬尖晶石接触; d—方辉橄榄岩中粗粒斜方辉石内部的橄榄石和铬尖晶石包体; e—方辉橄榄岩中自形的铬尖晶石; f—方辉橄榄岩中铬尖晶石产于斜方辉石内部并与橄榄石接触; g—方辉橄榄岩中橄榄石颗粒间的铬尖晶石; h—方辉橄榄岩中铬尖晶石内部的橄榄石包体; i—纯橄岩中的铬尖晶石; j—方辉橄榄岩中产于斜方辉石中的单斜辉石; k—方辉橄榄岩橄榄石中的单斜辉石呈针状出溶微晶; l—方辉橄榄岩中铬尖晶石的橄榄石和斜方辉石包体；Ol—橄榄石, Opx—斜方辉石, Cpx—单斜辉石, Sp—铬尖晶石
Figure 4. Microphotographs and back-scattered electron (BSE) images(j-l)of Dongqaio mantle peridotite Ol-Olivine, Opx-Orthopyroxene, Cpx-Clinopyroxene, Sp-Spinel
a-Porphyritic olivine embedded between orthopyroxenes in harzburgites; b-Olivine roundly enclosed in the orthopyroxene in harzburgites; c-Orthopyroxene in contact with spinel with harbor-shaped edge in harzburgites; d-Olivine and spinel in coarse-grained orthopyroxene in harzburgites; e-Euhedral spinel in harzburgites; f-Spinel enclosed in orthopyroxene and in contact with olivine in harzburgites; g-Spinel between olivines in harzburgites; h-Olivine enclosed in spinel in harzburgites; i-Spinel in dunites; j-Clinopyroxene enclosed in olivine in harzburgites; k-Exsolution lamella of clinopyroxene within orthopyroxene in harzburgites; l-Olivine and orthopyroxene enclosed by spinel in harzburgites
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图 5 东巧地幔橄榄岩橄榄石成分图解
地幔橄榄石序列据Takahashi, 1986；部分熔融趋势线据Ozawa, 1994；深海地幔橄榄岩及弧前地幔橄榄岩据Pagé et al., 2008；罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005
Figure 5. Compositional variations of olivines in peridotites of the Dongqiao ophiolite
The mantle olivine array after Takahashi, 1986; partial melting trends after Ozawa, 1994; abyssal peridotite and fore-arc peridotite after Pagé et al., 2008; Luobusha peridotites data (after Xu, 2009)); Bangonghu peridotites data (after Shi, 2005)
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图 6 东巧地幔橄榄岩斜方辉石成分图解(据Lian et al., 2016)
(罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)
Figure 6. Compositional variations of orthopyroxenes in peridotites of the Dongqiao ophiolite (after Lian et al., 2016)
Luobusha peridotite data (after Xu, 2009); Bangonghu peridotite data (after Shi, 2005)
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图 7 东巧地幔橄榄岩单斜辉石成分图解(据Lian et al., 2016)
(罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)
Figure 7. Compositional variations of chliopyroxenes in peridotites of the Dongqiao ophiolite (after Lian et al., 2016)
(Luobusha peridotite data after Xu, 2009; Bangonghu peridotite after Shi, 2005)
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图 8 东巧地幔橄榄岩尖晶石成分图解(据Pearce et al., 2000; Tamura and Aria, 2006; Lian et al., 2016)
(罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)MORB—大洋中脊型玄武岩; BON—玻安岩; FMM—富集的大洋中脊型地幔; IAT—岛弧拉斑质玄武岩
Figure 8. Compositional variations of spinels in peridotites of the Dongqiao ophiolite (after Pearce et al., 2000; Tamura and Aria, 2006; Lian et al., 2016)
Luobusha peridotite data (after Xu, 2009); Bangonghu peridotite data (after Shi, 2005) MORB-Mid-ocean ridge basalt; BON-Boninite; FMM-Fertile MOR mantle; IAT-Island arc tholeiite
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图 9 东巧地幔橄榄岩全岩Al2O3/SiO2-MgO/SiO2图解(据Lian et al., 2016)
(地球序列据Jagoutz et al., 1979; 深海地幔橄榄岩和弧前地幔橄榄岩据Hattori and Guillot, 2007;原始地幔据McDonough and Sun, 1995; 罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)
Figure 9. Whole rock weight ratios of Al2O3/SiO2-MgO/SiO2 diagram of mantle peridotites from Dongqiao ophiolite (after Lian et al., 2016)
Terrestrial array after Jagoutz et al., 1979; abyssal peridotite and forearc peridotite after Hattori and Guillot, 2007; primitive mantle after McDonough and Sun, 1995; Luobusha peridotite data (after Xu, 2009)); Bangonghu peridotite data (after Shi, 2005)
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图 10 东巧、班公湖、罗布莎地幔橄榄岩球粒陨石标准化稀土元素配分图(标准化值据McDonough and Sun, 1995; 据Lian et al., 2016)
(图中灰色区域代表深海地幔橄榄岩变化范围据Niu, 2004；粉色区域代表Izu-Bonin-Mariana弧前地幔橄榄岩的变化范围据Parkinson and Pearce, 1998；图中黑线代表尖晶石相地幔源区在近分离熔融模型经过2%~20%熔体提取后的熔融残余据Krishnakanta Singh, 2013；罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)
Figure 10. Chondrite-normalized REE patterns (normalization values after McDonough and Sun, 1995) for the peridotites from Dongqaio ophiolite (after Lian et al., 2016)
The gray region represents compositional variations of abyssal peridotites (after Niu, 2004); the pink region represents compositional variations of fore-arc peridotites from Izu-Bonin-Mariana (after Parkinson and Pearce, 1998); the dash lines are the range of model residual mantle compositions calculated using the modelling of nearfractional melting for different amounts of melt extraction (2%-20%) melting within the spinel stability field (after Krishnakanta Singh, 2013); Luobusha peridotite data (after Xu, 2009); Bangonghu peridotite data (after Shi, 2005)
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图 11 东巧、班公湖、罗布莎地幔橄榄岩原始地幔标准化微量元素蜘蛛图(标准化值据McDonough and Sun, 1995; 罗布莎数据据徐向珍, 2009；班公湖数据据史仁灯, 2005)
Figure 11. Primitive mantle-normalized trace elements patterns (normalization values after McDonough and Sun, 1995) for the peridotites from Dongqiao ophiolite Luobusha peridotite data (after Xu, 2009); Bangonghu peridotite data (after Shi, 2005)
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图 12 东巧地幔橄榄岩Tb/Yb-Al2O3图解(据Krishnakanta Singh, 2013)
Figure 12. Plot of Tb/Yb versus Al2O3 for peridotites from Dongqaio ophiolite (after Krishnakanta Singh, 2013)
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图 13 东巧蛇绿岩中地幔橄榄岩Sc-Ni(a)；Al2O3-Ni(b)；Ti-Ni(c)；Zr-Ni(d)图解(据Pearce et al., 2000)
Figure 13. Plots of Sc(a), Al(b), Ti(c) and Zr(d) against Ni for peridotites from Dongqaio ophiolite with partial melting trends (after Pearce et al., 2000)
表 1 东巧地幔橄榄岩中橄榄石的电子探针分析结果(部分数据)(%)
Table 1 Representative microprobe analyses of olivines from the Dongqiao mantle peridotites(%)
下载: 导出CSV
表 2 东巧地幔橄榄岩中斜方辉石的电子探针分析结果(部分数据)(%)
Table 2 Representative microprobe analyses of orthopyroxenes from the Dongqiao mantle peridotites(%)
下载: 导出CSV
表 3 东巧地幔橄榄岩中单斜辉石的电子探针分析结果(部分数据)(%)
Table 3 Representative microprobe analyses of clinopyroxenes from the Dongqiao mantle peridotites(%)
下载: 导出CSV
表 4 东巧地幔橄榄岩中铬尖晶石的电子探针分析结果(部分数据)(%)
Table 4 Representative microprobe analyses of spinels from the Dongqiao mantle peridotites(%)
下载: 导出CSV
表 5 东巧蛇绿岩地幔橄榄岩全岩地球化学分析数据(主量元素/%，稀土元素和微量元素/10−6)
Table 5 Whole rock composition of Dongqaio peridotites (Major elements: wt%; Rare Earth Elements and trace elements: ×10−6)
下载: 导出CSV
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