东天山梅岭铜矿床黄铁矿Re-Os等时线年龄:Os同位素不均一的结果

赵冰爽; 李杰; 龙晓平; 袁超

doi:10.3799/dqkx.2018.168

东天山梅岭铜矿床黄铁矿Re-Os等时线年龄:Os同位素不均一的结果

doi: 10.3799/dqkx.2018.168

赵冰爽^1,2,,
李杰^1, ,,
龙晓平^3, ,,
袁超¹

1.
中国科学院广州地球化学研究所同位素地球化学国家重点实验室, 广东广州 510640
2.
中国科学院大学, 北京 100049
3.
西北大学地质系, 大陆动力学国家重点实验室, 陕西西安 710069

基金项目:

国家自然科学基金项目 41373034

国家重点基础研究发展计划（973计划）项目 2014CB440801

国家自然科学基金项目 41522202

详细信息

作者简介:
赵冰爽(1994-), 女, 硕士研究生, 主要从事地球化学方面的研究

通讯作者:
李杰

龙晓平

中图分类号: P611
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- 被引次数: 0
出版历程
- 收稿日期: 2018-01-23
- 刊出日期: 2018-09-15

Re-Os Isochron Age of Pyrites from Meiling Cu Deposit in the Eastern Tianshan: A Case Study for the Os Isotopic Heterogeneity

Zhao Bingshuang^{1,2
,},
Li Jie^{1
, ,},
Long Xiaoping^{3
, ,},
Yuan Chao¹

1.
State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou 510640, China
2.
University of Chinese Academy of Sciences, Beijing 100049, China
3.
State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi'an 710069, China

摘要

摘要: 金属硫化物Re-Os等时线年龄的合理解释是揭示金属矿床成矿时代的关键.通过对新疆东天山梅岭铜矿床开展Re-Os同位素定年研究，结果表明浸染状和脉状矿石中黄铁矿样品在Os浓度和Os同位素比值方面都有很大的变化，这两类样品定义了很好的Re-Os等时线年龄，分别为523±59 Ma和707±99 Ma.由于得到的等时线年龄明显老于它们的实际地质成矿年龄，且¹⁸⁷Os/¹⁸⁸Os与普通Os的倒数（以1/¹⁹²Os为例）之间存在着很好的相关性（R²分别为0.997 3和0.994 5），因此这些样品存在着初始Os同位素组成不均一的现象，这些Re-Os等时线是混合等时线，没有地质意义.理论和数学公式推导显示观测到的Re-Os等时相关性是在形成时期没有达到完全的同位素平衡的二元混合的结果，这种同位素扩散不平衡产生的原因主要是在矿床形成时期Os同位素在金属硫化物与硅酸盐矿物之间的同位素扩散存在限制性.回归得到的Os的初始值更偏向于地壳值，表明矿床形成时期的地壳混染可能造成金属硫化物体系中的这种初始Os同位素不均一.因此，将Re-Os同位素体系应用于金属硫化物样品定年时，¹⁸⁷Os/¹⁸⁸Os与1/¹⁹²Os之间是否存在相关关系可以作为Re-Os等时线年龄是否具有地质意义的判断标准.
- 金属硫化物 /
- Re-Os同位素 /
- 初始Os同位素 /
- 等时线年龄 /
- 混合等时线 /
- 年代学
Abstract: Interpretations of the Re-Os isochron age of metallic sulfides are crucial to the reconstruction of ore-formation age of metallic deposits. Re-Os dating of pyrites from Meiling Cu deposit in eastern Tianshan, NW China indicates that the disseminated and massive ores show large variations in both Os concentrations and isotopic ratios. Our isotopic data of the two kinds of ores have defined good Re-Os correlations and the isochron ages are 523±59 Ma and 707±99 Ma, respectively. The two isochron ages are both significantly older than the true formation age of the Meiling Cu deposit. Together with the good correlations between ¹⁸⁷Os/¹⁸⁸Os ratio and the reciprocal of the common Os (i.e., 1/¹⁹²Os, R² are 0.997 3 and 0.994 5 for the disseminated and massive ores, respectively), we suggest that the initial Os isotopic compositions of these samples are heterogeneous and the two ages are mixed isochron ages. The mathematical deduction demonstrates that the observed Re-Os isochron correlations are the result of binary mixing without complete isotopic equilibrium at the time of formation, primarily due to limited diffusional exchange of Os isotopes between refractory Os-bearing inclusions and silicate minerals. The initial Os isotopic compositions may approach the value of continental crust. Crustal contamination during the formation of the deposit was responsible for the initial Os isotopic heterogeneity in the metallic sulfide system. It is concluded that whether there is a good Re-Os isochron correlation for samples can be used to constrain the geological meaning of Re-Os isochron ages when the Re-Os isotopic system of metallic sulfides is used to date the formation age of metallic deposit.
- metallic sulfide /
- Re-Os isotope /
- initial Os isotope /
- isochron age /
- mixed isochron /
- geochronolgy

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图 1 东天山地质概况

据Deng et al.(2016a)修改

Fig. 1. Geological sketch and distribution of the Cu-polymetallic deposits in the eastern Tianshan

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图 2 卡拉塔格地区地质概况

据Deng et al.(2016a)修改

Fig. 2. Regional geological sketch of the Kalatag area

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图 3 梅岭铜矿床两种类型矿石手标本照片

样品16HS0113和16HS0115为浸染状矿石；样品16HS0205和16HS0207为脉状矿石

Fig. 3. Photographs showing two kinds of ores from the Meiling Cu deposit

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图 4 梅岭铜矿两种类型矿石显微镜下照片

a.浸染状矿石镜下单偏光照片；b~d.脉状矿石镜下单偏光照片.浸染状矿石中黄铁矿颗粒离散分布于硅酸盐矿物中，脉状矿石中黄铁矿颗粒离散分布于黄铜矿或者硅酸盐矿物中

Fig. 4. Photomicrographs of copper ores from the Meiling Cu deposit

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图 5 梅岭铜矿床5个浸染状样品等时线图解(a)；梅岭铜矿床5个浸染状样品¹⁸⁷Os/¹⁸⁸Os-1/¹⁹²Os图解(b); 梅岭铜矿床5个脉状样品等时线图解(c)；梅岭铜矿床5个脉状样品¹⁸⁷Os/¹⁸⁸Os-1/¹⁹²Os图解(d)

Fig. 5. ¹⁸⁷Re/¹⁸⁸Os vs.¹⁸⁷Os/¹⁸⁸Os (a) and inverse of ¹⁹²Os (b) for pyrite samples from the disseminated ores; ¹⁸⁷Re/¹⁸⁸Os vs.¹⁸⁷Os/¹⁸⁸Os (c) and inverse of ¹⁹²Os (d) for pyrite samples from the vein ores

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图 6 Re-Os混合等时线

图据Li et al.(2014).a.k=0，具有不相同¹⁸⁷Os/¹⁸⁸Os比值的两端元混合过程中Os同位素交换达到了平衡或来自一个Os同位素均一的端元；在这种情况下，获得的等时线为传统意义上的等时线(A_p)，初始¹⁸⁷Os/¹⁸⁸Os线为I_p，等时线年龄(t_p)等于岩石形成的真实年龄(t).b.k≠0，具有不相同¹⁸⁷Os/¹⁸⁸Os比值的两端元混合过程中Os同位素交换没有达到平衡；在这种情况下获得的混合等时线(A_p)和初始混合线(I_M)以及真实形成年龄(t).获得的混合等时线的年龄(t_p)已经没有地质意义

Fig. 6. Illustration of binary mixing on the Re-Os isochron diagram

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图 7 (a) Haynes-Stellite矿床辉钴矿样品等时线图解；(b) Haynes-Stellite矿床辉钴矿样品¹⁸⁷Os/¹⁸⁸Os与1/¹⁹²Os图解; (c) Idaho地区4个辉钴矿样品等时线图解；(d) Idaho地区4个辉钴矿样品¹⁸⁷Os/¹⁸⁸Os与1/¹⁹²Os图解

Fig. 7. ¹⁸⁷Re/¹⁸⁸Os vs.¹⁸⁷Os/¹⁸⁸Os (a) and inverse of ¹⁹²Os (b) for samples from the Haynes-Stellite deposit; ¹⁸⁷Re/¹⁸⁸Os vs.¹⁸⁷Os/¹⁸⁸Os (c) and inverse of ¹⁹²Os (d) for samples from the Idaho zone

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图 8 Iimori矿床11个矿石样品等时线图解(a)；Iimori矿床11个矿石样品¹⁸⁷Os/¹⁸⁸Os与1/¹⁹²Os图解(b)

Fig. 8. ¹⁸⁷Re/¹⁸⁸Os vs.¹⁸⁷Os/¹⁸⁸Os (a) and inverse of ¹⁹²Os (b) for 11 samples from the Iimori deposit

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表 1 新疆梅岭铜矿床浸染状矿石黄铁矿Re-Os同位素分析数据

Table 1. Re-Os isotopic data of pyrite samples from the disseminated ores

样品编号	质量(g)	Re(10^-12)	±2σ(10^-12)	Os(10^-12)	±2σ(10^-12)	¹⁸⁷Os/¹⁸⁸Os	±2σ	¹⁸⁷Re/¹⁸⁸Os	±2σ	1/¹⁹²Os	T_MA(Ma)
16HS0104	0.593 4	2 424	26	15.28	0.16	50.771 1	0.709 5	5 815.45	88.96	1.234 6	520
16HS0107	0.605 2	2 174	116	13.67	0.28	54.922 5	1.540 2	6 244.42	130.37	1.478 2	524
16HS0108	0.605 5	2 718	25	26.53	0.10	8.519 0	0.079 3	1 033.95	10.41	0.194 6	485
16HS0113	0.611 6	3 827	40	23.32	0.10	43.997 2	0.403 9	5 314.68	60.51	0.714 5	493
16HS0115	0.606 0	2 885	29	18.43	0.07	33.558 0	0.298 8	4 043.74	43.77	0.720 5	494

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表 2 新疆梅岭铜矿床脉状矿石黄铁矿Re-Os同位素分析数据

Table 2. Re-Os isotopic data of pyrite samples from the vein ores

样品编号	质量(g)	Re(10^-12)	±2σ(10^-12)	Os(10^-12)	±2σ(10^-12)	¹⁸⁷Os/¹⁸⁸Os	±2σ	¹⁸⁷Re/¹⁸⁸Os	±2σ	1/¹⁹²Os	T_MA(Ma)
16HS0205	0.604 9	3 101	26	19.34	0.10	61.04	0.54	6 911.29	68.82	1.15	526
16HS0205	0.599 3	3 277	26	22.24	0.87	568.31	7.37	53 339.32	2 139.13	8.39	636
16HS0206	0.588 8	2 720	25	20.62	0.68	770.37	5.69	64 493.13	2 214.12	12.23	712
16HS0207	0.578 1	2 867	26	17.90	0.49	151.12	2.58	15 968.23	458.88	2.87	564
16HS0208	0.488 2	5 381	34	34.24	0.09	42.13	0.21	4 905.34	33.30	0.47	511

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