阿尔泰南缘乌拉斯沟铜矿床S-Pb-Sr-Nd-C-H-O同位素特征及其对成矿物质和流体来源限定

卢琦园; 郑义; 王成明; 王岳军

doi:10.3799/dqkx.2018.135

阿尔泰南缘乌拉斯沟铜矿床S-Pb-Sr-Nd-C-H-O同位素特征及其对成矿物质和流体来源限定

doi: 10.3799/dqkx.2018.135

卢琦园^1,2,,
郑义^1,2, ,,
王成明^1,2,
王岳军^1,2

1.
中山大学地球科学与工程学院, 广东广州 510275
2.
广东省地质过程与矿产资源探查重点实验室, 广东广州 510275

基金项目:

珠江科技新星项目 201710010027

广东省引进人才创新创业团队项目 2016ZT06N331

国家自然科学基金项目 41502068

广东省自然科学基金杰出青年基金项目 2018B030306021

科技部国家重点研发计划项目 2016YFC0600408

详细信息

作者简介:
卢琦园(1995-), 男, 硕士研究生, 主要从事矿床学方面的研究

通讯作者:
郑义

中图分类号: P611
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- 被引次数: 0
出版历程
- 收稿日期: 2018-01-25
- 刊出日期: 2018-09-15

S-Pb-Sr-Nd-C-H-O Isotopic Geochemistry of the Wulasigou Cu Deposit in the South Altay: Constraints for the Fluid and Metal Sources

Lu Qiyuan^{1,2
,},
Zheng Yi^{1,2
, ,},
Wang Chengming^1,2,
Wang Yuejun^1,2

1.
School of Earth Science and Engineering, Sun Yat-sen University, Guangzhou 510275, China
2.
Guangdong Provincial Key Lab of Geological Processes and Mineral Resource Survey, Guangzhou 510275, China

摘要

摘要: 新疆乌拉斯沟铜矿床位于阿尔泰造山带南缘克兰盆地内，为近年来新发现的矿床，受NW向断裂控制的脉状矿体产于泥盆系康布铁堡组变质火山岩系中，目前其成矿流体和成矿物质来源尚不明确.在细致的矿床地质研究基础上，通过开展S-Pb-Sr-Nd-C-H-O同位素分析，根据野外和显微镜下观察，可将乌拉斯沟铜矿床的形成划分为黄铁矿-磁铁矿-石英、黄铜矿-绿泥石-绿帘石-石英及石英-碳酸盐阶段.同位素分析结果显示：乌拉斯沟铜矿硫化物样品δ³⁴S值为0.1‰~3.2‰，平均为1.6‰，落入未矿化围岩δ³⁴S值范围（-4.7‰~18.68‰），矿石硫可能源自康布铁堡组.成矿晚阶段的方解石样品δ¹³C_V-PDB‰=-1.1‰，δ¹⁸O_V-PDB‰=-20.3‰，海相碳酸盐地层和有机碳是可能的碳质来源.8件黄铁矿的Pb同位素为²⁰⁶Pb/²⁰⁴Pb=17.939~18.508（平均18.255），²⁰⁷Pb/²⁰⁴Pb=15.519~15.674（平均15.578），²⁰⁸Pb/²⁰⁴Pb=37.881~38.653（平均38.209），与康布铁堡组围岩类似.初始I_{Sr（220 Ma）}为0.710 4~0.711 7，平均值为0.711 1，初始¹⁴³Nd/¹⁴⁴Nd值为0.512 002~0.512 240（平均0.512 103）.矿石Sr-Nd-Pb同位素组成均指示乌拉斯沟铜矿成矿物质可能主要源自围岩康布铁堡组，并可能有外来成矿物质的加入.流体的δD_V-SMOW变化于-103.8‰~-92‰（平均值为-99.2‰），石英和方解石矿物的δ¹⁸O_V-SMOW值集中在9.4‰~11.5‰（平均值为10.4‰），δ¹⁸O_H₂O值为2.1‰~4.2‰（平均值为3.1‰），结合流体包裹体物理化学特征，成矿热液可能来源于变质水，但可能受到大气降水的影响而偏移.因此，乌拉斯沟铜矿成矿物质主要来源于赋矿围岩的变质脱挥发分作用，这与造山型矿床的成矿机制吻合.
- 乌拉斯沟铜矿 /
- 造山型矿床 /
- 阿尔泰造山带 /
- 同位素 /
- 地球化学
Abstract: The Wulasigou Cu deposit is a recent discovered ore deposit, located in Devonian volcanic-sedimentary basin of the Altay orogenic belt. Vein-shaped orebodies are hosted in the Kangbutiebao Formation and controlled by the NW-trending faults. In order to investigate the origin of ore-forming fluid and metal, a series of S-Pb-Sr-Nd-C-H-O isotopic analysis was carried out. According to field work and microscopic observation, the mineralization stages of the Wulasigou Cu deposit can be divided into pyrite-magnetite-quartz, chalcopyrite-chlorite-epidote-quartz and quartz-carbonate stages. The δ³⁴S values of sulfide samples in this deposit are 0.1‰-3.2‰ (average:1.6‰), falling into the range of the δ³⁴S values of wall rocks (-4.7‰-18.68‰), indicating that sulfur may be mainly derived from the Kangbutiebao Formation. The calcite sample shows δ¹³C_V-PDB‰=-1.1‰ and δ¹⁸O_V-PDB‰=-20.3‰, indicating that the marine carbonate strata and organic carbon are probably the sources of carbon. The Pb isotopes of eight pyrite samples are ²⁰⁶Pb/²⁰⁴Pb=17.939-18.508 (average 18.255), ²⁰⁷Pb/²⁰⁴Pb=15.519-15.674 (average 15.578), ²⁰⁸Pb/²⁰⁴Pb=37.881-38.653 (average 38.209), similar to those of the Kangbutiebao Formation. The I_{Sr(220 Ma)} values of pyrite are 0.710 4-0.711 7 (average 0.711 1), with initial ¹⁴³Nd/¹⁴⁴Nd values of 0.512 002-0.512 240 (average 0.512 103). The Sr-Nd-Pb isotopic compositions indicate that the metal sources of Wulasigou Cu deposit may be mainly from the Kangbutiebao Formation but with additional minerals. The δD_V-SMOW values of the fluid range from -103.8‰ to -92‰ (average -99.2‰), the δ¹⁸O_V-SMOW values for quartz and calcite are concentrated at 9.4‰-11.5‰ (average 10.4‰), and the δ¹⁸O_H₂O values range from 2.1‰ to 4.2‰ (average 3.1‰), indicating that the hydrothermal fluids may be originated from metamorphic water with the effect of meteoric water combined with physical and chemical characteristics of fluid inclusions. The metallogenic material of the Wulasigou Cu deposit is mainly derived from the metamorphic devolatilization of the host rock, which is consistent with the ore-forming mechanism of the orogenic deposit.
- Wulasigou Cu deposit /
- orogenic deposit /
- Altay orogenic belt /
- isotope /
- geochemistry

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图 1 研究区大地构造背景和区域地质及矿产分布

a.研究区大地构造背景；b.阿尔泰南缘阿尔泰南缘克兰盆地区域地质及矿产分布.据Zheng et al.(2012)及其引文

Fig. 1. Tectonic background and regional geology and mineral distribution of the study area

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图 2 乌拉斯沟铜矿床矿区地质简图(a)及A1-A2勘探线剖面(b)

据Zheng et al.(2012)及其引文

Fig. 2. Geological sketch and exploration line A1-A2 of the Wulasigou Cu deposit

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图 3 乌拉斯沟铜矿床硫同位素组成

Fig. 3. S isotopic composition of pyrite and wall rocks in the Wulasigou Cu deposit

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图 4 乌拉斯沟铜矿床成矿流体δ¹⁸O-δD组成

底图据Taylor(1974)

Fig. 4. δ¹⁸O-δD isotopic composition of the ore-forming fluid in the Wulasigou Cu deposit

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图 5 乌拉斯沟铜矿金属硫化物及围岩初始Sr、Nd同位素图解

Fig. 5. Initial Sr-Nd isotopic composition of sulfides and wall rocks in the Wulasigou deposit

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图 6 乌拉斯沟矿石硫化物及围岩铅同位素图解

Fig. 6. Pb isotopic diagram of sulfides and wall rocks of the Wulasigou Cu deposit

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表 1 乌拉斯沟铜矿床硫化物及围岩硫同位素组成

Table 1. S isotopic composition of sulfide and wall rocks in the Wulasigou Cu deposit

序号	样品编号	δ³⁴S_V-CDT(‰)	测试样品	数据来源
1	10WL-09	1.7	黄铁矿	本文
2	10WL-12	2.9	黄铁矿	本文
3	10WL-Q5B	2.0	黄铁矿	本文
4	10WL-13	3.2	黄铁矿	本文
5	10WL-Q1	1.0	黄铁矿	本文
6	10WL-Q8B	0.7	黄铁矿	本文
7	10WL-Q4	0.1	黄铁矿	本文
8	10WL-Q3	1.3	黄铁矿	本文
9	10TMZK-34A	5.6	无矿化大理岩	Niu et al., 2017
10	SL-30	7.5	无矿化绿片岩	Niu et al., 2017
11	TM-26	7.5	未矿化大理岩	Niu et al., 2017
12	SL-38	16.5	未矿化凝灰岩	Niu et al., 2017
13	SL-37	16.4	未矿化凝灰岩	Niu et al., 2017
14	SL-15	18.7	未矿化凝灰岩	Niu et al., 2017
15	10DD-13	-4.7	无矿化灰岩	Niu et al., 2017
16	TM-51	-19.3	矿化绿泥片岩	Niu et al., 2017
17	TM-01	-24.1	浸染矿化砂岩	Niu et al., 2017
18	TM-06	-16.8	矿化绿泥片岩	Niu et al., 2017
19	TM-14	-13.7	矿化绿泥片岩	Niu et al., 2017

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表 2 乌拉斯沟铜矿床氢氧同位素组成

Table 2. δ¹⁸O-δD isotopic composition of quartz in the Wulasigou Cu deposit

序号	样品编号	岩性	δD_V-SMOW(‰)	δ¹⁸O_V-SMOW(‰)	δ¹⁸O_H₂O(‰)	T(℃)
1	WL-Q1	石英	/	9.4	2.1	289
2	WL-Q3	石英	-103.8	10.8	3.5	289
3	WL-Q4	石英	-103.7	10.4	3.1	289
4	WL-Q8B	石英	/	10.1	2.8	289
5	WL-13	石英	-92.0	10.5	3.2	289
6	WL-09	石英	/	10.7	3.4	289
7	WL-12	石英	-94.8	11.5	4.2	289
8	WL-Q5B	石英	-101.6	9.7	2.4	289

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表 3 乌拉斯沟铜矿床碳同位素组成

Table 3. C isotopic composition of the Wulasigou Cu deposit

样品编号	矿物/岩石	δ¹³C_V-PDB(‰)	δ¹⁸O_V-PDB(‰)	δ¹⁸O_V-SMOW(‰)	数据来源
10WL-0-5C	方解石	-1.1	-20.3	9.9	本文
DDZK-7	大理岩	-1.2	-15.8	14.7	Niu et al., 2017
10TMZK-37B	大理岩	2.7	-18.5	11.9	Niu et al., 2017
10TMZK-34A	大理岩	2.2	-20.5	9.7	Niu et al., 2017
10DD-13	灰岩	-1.6	-15.8	14.6	Niu et al., 2017
10SK-11A	灰岩	-1.7	-16.3	14.1	Niu et al., 2017
注：本次测试只获得1件成矿晚阶段的方解石样品(样品编号10WL-0-5C)，δ¹³C_V-PDB(‰)=-1.1‰，δ¹⁸O_V-PDB(‰)=-20.3‰.Niu et al.(2017)获得围岩C同位素值介于-1.7‰~2.7‰(平均值为2.1‰)，其中大理岩δ¹³C_V-PDB为-1.2‰~2.7‰(平均值为1.2‰)，灰岩δ¹³C_V-PDB为-1.6‰~-1.7‰(平均值-1.7‰).

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表 4 乌拉斯沟矿床金属硫化物及围岩Sr同位素组成

Table 4. Sr isotopic composition of sulfides and wall rocks in the Wulasigou deposit

样品号	样品名称	Rb(10^-6)	Sr(10^-6)	⁸⁷Rb/⁸⁶Sr	⁸⁷Sr/⁸⁶Sr	I_{Sr(220 Ma)}
10WL-09	黄铁矿	0.03	0.37	0.246 8	0.712 3	0.711 6
10WL-12	黄铁矿	0.13	1.52	0.239 4	0.712 0	0.711 3
10WL-Q5B	黄铁矿	0.09	1.16	0.229 4	0.712 4	0.711 7
10WL-13	黄铁矿	0.24	0.79	0.889 4	0.713 6	0.710 8
10WL-Q1	黄铁矿	0.05	0.68	0.194 4	0.712 0	0.711 4
10WL-Q8B	黄铁矿	0.10	1.42	0.207 0	0.710 7	0.710 1
10WL-Q4	黄铁矿	0.04	0.73	0.160 6	0.710 9	0.710 4
10WL-Q3	黄铁矿	0.05	0.51	0.278 0	0.712 4	0.711 5
	平均值(n=8)					0.711 1

样品号	样品名称	Rb(10^-6)	Sr(10^-6)	⁸⁷Rb/⁸⁶Sr	⁸⁷Sr/⁸⁶Sr	I_{Sr(220 Ma)}
10SKY-09	方解石	0.14	341.0	0.001 2	0.720 5	0.720 5
10SKY-07	方解石	0.13	459.0	0.000 8	0.717 3	0.717 3
10SKY-05	方解石	0.22	511.0	0.001 3	0.714 2	0.714 2
10SKY-02	方解石	0.06	315.0	0.000 6	0.717 2	0.717 2
10TMZK	大理岩	0.84	103.0	0.023 6	0.713 1	0.713 0
10DD-13	灰岩	107.00	372.0	0.833 5	0.710 9	0.708 3
10TM-11	晶屑凝灰岩	97.80	12.3	23.08 5	0.809 8	0.737 6
10SK-10	晶屑凝灰岩	51.10	33.4	4.429 4	0.742 3	0.728 5
10SK-3a	钙质粉砂岩	146.00	49.8	8.467 1	0.754 2	0.727 7
SL-30	绿片岩	6.98	348.0	0.058 1	0.711 8	0.711 6
	平均值(n=10)					0.719 6
注：表中的⁸⁷Rb/⁸⁶Sr是根据实测的样品元素含量和同位素比值计算所得，成矿年龄采用黑云母Ar-Ar年龄220 Ma(Zheng et al., 2012)，将测得的⁸⁷Sr/⁸⁶Sr同位素比值返算回220 Ma时的⁸⁷Sr/⁸⁶Sr比值I_{Sr(220 Ma)}；初始Sr计算公式：I_Sr=(⁸⁷Sr/⁸⁶Sr)_m-(⁸⁷Rb/⁸⁶Sr)_m(e^λt-1).

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表 5 乌拉斯沟铜矿金属硫化物及围岩Nd同位素组成

Table 5. Nd isotopic composition of sulfides and wall rocks in the Wulasigou deposit

样品号	样品名称	Sm(10^-6)	Nd(10^-6)	¹⁴⁷Sm/¹⁴⁴Nd	¹⁴³Nd/¹⁴⁴Nd	(¹⁴³Nd/¹⁴⁴Nd)_i	ε_Nd
10WL-09	黄铁矿	0.35	1.00	0.209 1	0.512 444	0.512 143	-9.7
10WL-12	黄铁矿	0.22	0.80	0.161 5	0.512 473	0.512 240	-7.8
10WL-Q5B	黄铁矿	0.09	0.25	0.204 4	0.512 387	0.512 093	-10.6
10WL-13	黄铁矿	0.39	2.19	0.106 0	0.512 325	0.512 172	-9.1
10WL-Q1	黄铁矿	0.05	0.20	0.139 5	0.512 233	0.512 031	-11.8
10WL-Q8B	黄铁矿	0.24	1.23	0.120 4	0.512 260	0.512 087	-10.8
10WL-Q4	黄铁矿	0.17	0.67	0.148 3	0.512 216	0.512 002	-12.4
10WL-Q3	黄铁矿	0.05	0.19	0.168 0	0.512 300	0.512 058	-11.3
	平均值(n=8)					0.512 103	-10.4
10SKY-09	方解石	0.16	0.53	0.179 1	0.512 470	0.512 212	-12.4
10SKY-07	方解石	0.25	0.63	0.239 9	0.512 681	0.512 336	-11.4
10SKY-05	方解石	1.04	2.79	0.225 1	0.512 632	0.512 308	-11.6
10SKY-02	方解石	0.54	1.28	0.254 8	0.512 640	0.512 273	-13.0
10TMZK	大理岩	0.43	1.87	0.140 0	0.512 450	0.512 248	-10.8
10DD-13	灰岩	3.73	18.6	0.121 7	0.512 322	0.512 147	-12.4
10TM-11	晶屑凝灰岩	3.09	15.8	0.117 9	0.512 550	0.512 380	-7.7
10SK-10	晶屑凝灰岩	7.82	39.8	0.118 7	0.512 499	0.512 328	-8.8
10SK-3a	钙质粉砂岩	7.24	36.8	0.119 1	0.512 559	0.512 388	-7.6
SL-30	绿片岩	4.27	15.2	0.169 8	0.512 881	0.512 636	-3.9
	平均值(n=10)					0.512 326	-10.2
注：表中的¹⁴⁷Sm/¹⁴⁴Nd是根据实测的样品元素含量和同位素比值计算所得，成矿年龄采用黑云母Ar-Ar成矿年龄220 Ma(Zheng et al., 2012)，将测得的¹⁴³Nd/¹⁴⁴Nd同位素比值返算回220 Ma时的(¹⁴³Nd/¹⁴⁴Nd)_{i(220 Ma)}和ε_Nd(t)值；初始Nd计算公式：(¹⁴³Nd/¹⁴⁴Nd)=(¹⁴³Nd/¹⁴⁴Nd)_m-(¹⁴⁷Sm/¹⁴⁴Nd)_m(e^λt-1)，其中λ=0.006 54×10^-9 a^-1.计算过程中，球粒陨石均一储库(CHUR)_Nd同位素参数采用¹⁴³Nd/¹⁴⁴Nd=0.512 638(Goldstein et al., 1984)，¹⁴⁷Sm/¹⁴⁴Nd=0.196 7(Jacobsen and Wasserburg, 1984).

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表 6 乌拉斯沟矿床金属硫化物及围岩Pb同位素组成

Table 6. Pb isotopic composition of sulfides and wall rocks in the Wulasigou deposit

样品号	样品名称	²⁰⁶Pb/ ²⁰⁴Pb	²⁰⁷Pb/ ²⁰⁴Pb	²⁰⁸Pb/ ²⁰⁴Pb
10WL-09	黄铁矿	18.255	15.570	38.123
10WL-12	黄铁矿	18.449	15.648	38.537
10WL-Q5B	黄铁矿	18.199	15.519	37.888
10WL-13	黄铁矿	18.455	15.674	38.653
10WL-Q1	黄铁矿	18.508	15.611	38.436
10WL-Q8B	黄铁矿	18.087	15.545	37.881
10WL-Q4	黄铁矿	18.145	15.526	37.901
10SK-06	黄铁矿	17.939	15.528	38.250
	平均值(n=8)	18.255	15.578	38.209
10TMZK	大理岩	18.066	15.510	37.762
10DD-13	灰岩	18.102	15.506	37.813
10TM-11	晶屑凝灰岩	18.651	15.551	38.576
10SK-10	晶屑凝灰岩	18.674	15.551	38.541
10SK-3a	钙质粉砂岩	18.850	15.584	38.707
SL-30	绿片岩	18.265	15.528	38.070
	平均值(n=6)

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参考文献(65)

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