台湾利吉混杂岩中蛇纹岩岩石学和U-Pb年代学及其地质意义

耿威; 张训华; 刘昌岭; 孙治雷; 孙建业; 尚鲁宁; 马雪

doi:10.16562/j.cnki.0256-1492.2018.02.013

台湾利吉混杂岩中蛇纹岩岩石学和U-Pb年代学及其地质意义

1.
中国地质调查局青岛海洋地质研究所，青岛 266071

2.
海洋国家实验室海洋矿产资源评价与探测技术功能实验室，青岛 266071

3.
国土资源部天然气水合物重点实验室，青岛 266071

4.
中国地质调查局南京地质调查中心，南京 210016

基金项目:
国家自然科学基金青年科学基金项目“台湾利吉混杂岩基性-超基性岩块来源与弧陆碰撞过程”(41506083)；“鱼山-久米断裂带构造特征及其对中新世纪以来东海东部构造演化的分隔控制”(41606050)；中国地质调查局地质调查计划项目(DD20160218)；国家重点基础研究发展计划课题“构造地质过程及其对热液活动的控制”(2013CB429700)；国家重点研发计划课题“水合物泄露流体原位监测技术与装置”(2017YFC0307704)

详细信息

作者简介: 耿威(1983—)，女，博士，主要从事海洋地质研究，E-mail：gengwei0128@aliyun.com

通讯作者: 张训华，男，研究院，博导，E-mail：xunhuazh@vip.sina.com

中图分类号: P546

蔡秋蓉编辑

收稿日期: 2016-11-17

修回日期: 2016-12-08

刊出日期: 2018-04-28

Petrology and U-Pb geochronology of the serpentinite in the Lichi mélange of Eastern Taiwan and their tectonic implications

1.
Qingdao Institute of Marine Geology, China Geological Survey, Qingdao 266071, China

2.
Laboratory for Marine Mineral Resources; Qingdao National Laboratory for Marine Science and Technology, Qingdao 266071, China

3.
The Key Laboratory of Gas Hydrate, Ministry of Land and Resources, Qingdao 266071, China

4.
Nanjing Center, China Geological Survey, Nanjing 210016, China

More Information

Corresponding author: ZHANG Xunhua, xunhuazh@vip.sina.com

Received Date: 17 November 2016

Revised Date: 08 December 2016

Publish Date: 28 April 2018

摘要

摘要:
台湾利吉混杂岩位于吕宋岛弧与欧亚大陆发生碰撞(弧陆碰撞)关键地带，是菲律宾海板块和欧亚板块结合带重点研究的区域，其中出露的蛇纹岩可以为研究弧陆碰撞造山过程提供重要细节信息。利吉混杂岩中蛇纹岩岩块原岩为橄榄岩，通过锆石U-Pb年代学分析，得到代表洋壳年龄的橄榄岩形成年龄为17.7±0.5Ma，结合南海洋壳、菲律宾海洋壳年龄和构造背景，判断利吉混杂岩中的蛇纹岩(蛇纹石化橄榄岩)来自马尼拉俯冲系统的弧前盆地，是在利吉混杂岩形成过程中经第二次逆冲混入利吉混杂岩系统的。明确蛇纹岩岩块来源可以为利吉混杂岩形成提供细节信息，为研究弧陆碰撞造山活动和板块运动提供可靠依据。
- 利吉混杂岩 /
- 蛇纹岩 /
- 弧陆碰撞 /
- U-Pb年代学 /
- 台湾
Abstract:
Lichi Mélange, located along the plate suture between the southeastern Eurasian Plate and the Philippine Sea Plate, is a research focus of the collision of the Luzon Arc with the Eurasian Continent. The serpentinite, as a key component of the Mélange, can provide important information for studying the arc-continent collision. Petrographic study suggests that the protolith of the serpentinite is peridotite and the zircon U-Pb chronology data reveals that the serpentinite was formed 17.7±0.5 Ma. The serpentinite or serpentinised peridotite is supposed to come from a forearc basin in the Manila subduction system, based on their ages and the evolution of the South China Sea and the Philippine Sea as well as their tectonic backgrounds, and became part of the mélange in the second thrust westward. The origin of serpentinite in the Lichi Mélange may provide detailed information and a reliable basis for the study of arc-continent collision orogenic activity and plate tectonic movement.
- the Lichi Mélange /
- serpentinite /
- arc-continent collision /
- U-Pb geochronology /
- Taiwan

HTML全文

图 1 研究区构造位置图及取样点(修改自文献[17, 27])

Figure 1.

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图 2 利吉混杂岩野外和CR-16蛇纹岩手标本照片

Figure 2.

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图 3 CR-16蛇纹岩镜下特征

Figure 3.

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图 4 CR-16蛇纹岩代表性锆石二次电子像(上)和阴极发光图像(下)

Figure 4.

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图 5 CR-16蛇纹岩U-Pb谐和曲线图解

Figure 5.

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图 6 蛇纹岩逆冲混入利吉混杂岩示意图

Figure 6.

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表 1 利吉混杂岩中蛇纹岩样品CR-16锆石U-Pb测年结果

Table 1. U-Pb data for zircons from sample CR-16 in the Lichi Mélange

点	Th/10^-6	U/10^-6	Th/U	²⁰⁷Pb/²³⁵U		²⁰⁶Pb/²³⁸U		rho	²⁰⁷Pb/²³⁵U		²⁰⁶Pb/²³⁸U
点	Th/10^-6	U/10^-6	Th/U	比值	1δ	比值	1δ	rho	年龄/Ma	1δ	年龄/Ma	1δ
01	8713.87	2810.29	3.10	0.08143	0.00912	0.00313	0.00011	0.30	79.5	8.6	20.1	0.7
02	6466.59	2652.85	2.44	0.03275	0.00247	0.00285	0.00008	0.37	32.7	2.4	18.4	0.5
03	10575.96	3150.27	3.36	0.02600	0.00212	0.00268	0.00007	0.31	26.1	2.1	17.3	0.4
04	1591.10	1144.91	1.39	0.06552	0.00564	0.00284	0.00011	0.46	64.4	5.4	18.3	0.7
05	1359.32	1035.28	1.31	0.09187	0.00840	0.00323	0.00013	0.43	89.2	7.8	20.8	0.8
06	9256.35	2992.29	3.09	0.04407	0.00721	0.00266	0.00007	0.17	43.8	7.0	17.1	0.5
07	4670.87	2517.91	1.86	0.03789	0.00317	0.00278	0.00008	0.34	37.8	3.1	17.9	0.5
08	9487.53	3031.67	3.13	0.03393	0.00251	0.00269	0.00007	0.33	33.9	2.5	17.3	0.4
09	4713.09	2374.17	1.99	0.03777	0.00316	0.00286	0.00009	0.36	37.6	3.1	18.4	0.5
10	5198.71	2315.43	2.25	0.03536	0.00288	0.00276	0.00009	0.39	35.3	2.8	17.8	0.6
11	7263.84	2725.53	2.67	0.03079	0.00279	0.00254	0.00007	0.31	30.8	2.7	16.4	0.5
12	5054.18	2641.81	1.91	0.03590	0.00287	0.00271	0.00007	0.34	35.8	2.8	17.4	0.5
13	10001.42	3030.82	3.30	0.03132	0.00217	0.00264	0.00007	0.40	31.3	2.1	17.0	0.5
14	9479.40	2983.29	3.18	0.02505	0.00163	0.00272	0.00008	0.44	25.1	1.6	17.5	0.5
15	7965.91	2853.24	2.79	0.02792	0.00175	0.00272	0.00007	0.41	28.0	1.7	17.5	0.5
16	6253.29	2158.81	2.90	0.04646	0.00332	0.00320	0.00016	0.68	46.1	3.2	20.6	1.0
18	2548.62	1318.04	1.93	0.06640	0.00725	0.00271	0.00011	0.37	65.3	6.9	17.4	0.7
19	4872.20	2505.01	1.94	0.03388	0.00259	0.00273	0.00008	0.39	33.8	2.5	17.6	0.5
20	2341.44	1263.88	1.85	0.05901	0.00809	0.00257	0.00012	0.34	58.2	7.8	16.6	0.8
注：实验在中国地质大学(武汉)地质过程与矿产资源国家重点实验室(GPMR)利用LA-ICP-MS同时分析完成，对分析数据的离线处理(包括对样品和空白信号的选择、仪器灵敏度漂移校正、元素含量及U-Th-Pb同位素比值和年龄计算)采用软件ICPMSDataCal^[29]完成，详细的仪器操作条件和数据处理方法同文献[29, 30]。

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