新疆富蕴县库额尔齐斯铁矿成因机制探讨研究

张超; 刘锋; 杨富全

新疆富蕴县库额尔齐斯铁矿成因机制探讨研究

1.
广东省地质局七一九地质大队，广东肇庆 526020

2.
国土资源部成矿作用与资源评价重点实验室，中国地质科学院矿产资源研究所，北京 100037

基金项目:
国家科技支撑计划项目(2011BAB06B03-02); 国土资源部公益性行业专项资金课题(200911007-10,200911043-02)

详细信息

作者简介: 张超，工程师，矿床学专业。E-mail: czcl719@sina.com

通讯作者: 刘锋，研究员，主要从事矿床地球化学的研究。E-mail: liufeng@cags.ac.cn

中图分类号: O657.63; P578.12

收稿日期: 2012-02-24

录用日期: 2012-10-24

A Discussion on Genetic Mechanism of the Kuerqis Iron Deposit in Fuyun County, Xinjiang

1.
No.719 Geological Party, Bureau of Geological Exploration of Guangdong Province, Zhaoqing 526020, China

2.
Key Laboratory of Metallogeny and Mineral Assessment, Ministry of Land and Resources, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China

More Information

Corresponding author: Fen LIU, liufeng@cags.ac.cn

Received Date: 24 February 2012

Accepted Date: 24 October 2012

摘要

摘要: 目前针对阿尔泰南缘一带的小型富铁矿床研究明显不足。本文研究了库额尔齐斯富铁矿的成矿时代及成矿机制，为区域铁成矿规律和成矿预测提供基础资料。野外地质调查表明，该矿床地质特征具有火山沉积成因，但主要与花岗斑岩侵入的热液活动有关，二长花岗岩对铁矿有破坏作用。利用激光剥蚀-多接收器电感耦合等离子体质谱法测定了矿区两个花岗岩体的年龄，利用同位素质谱计测定了矿床中黄铁矿的硫同位素组成，分析表明花岗斑岩锆石18个测点在谐和线上成群分布，²⁰⁶Pb/²³⁸U年龄值集中在273～282.6 Ma，加权平均年龄为(278.7±0.94) Ma(MSDW=1.6)；二长花岗岩12个测点集中成群分布，²⁰⁶Pb/²³⁸U年龄值集中在271.8～276.8 Ma，加权平均年龄为(274.1±1.1) Ma(MSDW=0.47)。黄铁矿的δ³⁴S值变化于-7.2‰～0.7‰，多为负值，但大多数集中在0值附近，表明深源岩浆在向上运移过程中可能与围岩或早期沉积铁矿发生了明显的硫同位素交换，暗示铁的富集成矿主要发生在花岗斑岩侵入的热液期。综合区域研究认为，矿区花岗岩均属于阿尔泰南缘广泛发育的早二叠世时期岩浆事件，形成于板内伸展拉张环境。该期岩浆活动也伴随了铁等广泛的金属成矿作用。
- LA-MC-ICP-MS U-Pb定年 /
- 硫同位素组成 /
- 岩浆热液成因 /
- 库额尔齐斯铁矿
Abstract: The large iron deposits in the southern margin of Altay had been studied systematically, but researches on some small Fe-rich type such as Kuerqis iron deposit are still obviously insufficient. In this paper, a study of the chronology and genetic mechanism to supply basic information for regional metallogeny and mineral assessment is documented. The Kuerqis iron deposit is located in the Erqis tectonic belt in the southern margin of Altay. The field investigation suggests that the deposit is dominantly related to hydrothermal activity of granitic porphyry besides the volcanic sedimentary genesis, meanwhile the iron deposit was destroyed by monzonitic granite. The ages of two granite intrusions in the deposit area and S isotope composition of pyrites in ore were determined by Laser Ablation-Multicollector Inductively Coupled Plasma-Mass Spectrometry (LA-MC-ICP-MS) and MAT 251 EM Mass Spectrograph. The ²⁰⁶Pb/²³⁸U ages of 18 data points of zircons in granitic porphyry concentrated on the concordia line range from 273 Ma to 282.6 Ma and the weighted average age is (278.7±0.94) Ma with MSDW=1.6. The ²⁰⁶Pb/²³⁸U ages of 12 data points of zircons in monzonitic granite concentrated on the concordia line range from 271.8 Ma to 276.8 Ma and the weighted average age is (274.1±1.1) Ma with MSDW=0.47. δ³⁴S in pyrites varies from -7.2‰ to 0.7‰ and most are negative and near 0. The characteristic of δ³⁴S perhaps reflects the significant exchange of S isotope between magma from deep source and wall-rocks or the earlier sedimentary iron deposit during ascending magma. The mineralization prominently occurred in the hydrothermal period of granitic porphyry. Combined with former studies, it suggested that two granite intrusions in the deposit area intruded in a plate extension environment during the early-Permian when granite intrusions developed widely in the southern margin of Altay. Moreover, the extensive mineralization of iron and other elements perhaps occurred in this granitic event.
- LA-MC-ICP-MS U-Pb dating /
- sulfur isotopic composition /
- granitic hydrothermalism /
- Kuerqis iron deposit

HTML全文

图 1 库额尔齐斯铁矿床地质图(矿区地质图据甘肃煤田一四五队修编，构造图据文献^[4]编绘)

Figure 1.

下载: 全尺寸图片幻灯片

图 2 花岗斑岩(a)和二长花岗岩(b)中锆石的阴极发光图像

Figure 2.

下载: 全尺寸图片幻灯片

图 3 花岗斑岩锆石LA-MC-ICP-MS U-Pb年龄谐和图

Figure 3.

下载: 全尺寸图片幻灯片

图 4 二长花岗岩锆石LA-MC-ICP-MS U-Pb年龄谐和图

Figure 4.

下载: 全尺寸图片幻灯片

图 5 库额尔齐斯铁矿硫同位素图解

Figure 5.

下载: 全尺寸图片幻灯片

表 1 矿区花岗斑岩和二长花岗岩锆石U-Pb定年数据

Table 1. The U-Pb dating data of granitic porphyry and monzonitic granite

花岗斑岩锆石U-Pb同位素分析数据
测点	w_B/(μg·g^-1)		Th/U	²⁰⁶Pb/²³⁸U		²⁰⁷Pb/²³⁵U		²⁰⁸Pb/²³²Th		²⁰⁷Pb/²⁰⁶Pb		²⁰⁶Pb/²³⁸U		²⁰⁷Pb/²³⁵U		²⁰⁷Pb/²⁰⁶Pb		谐和度
测点	U	Th	Th/U	比值	1σ	比值	1σ	比值	1σ	比值	1σ	年龄/Ma	1σ	年龄/Ma	1σ	年龄/Ma	1σ	谐和度
ker01-1	353.5	286.2	0.81	0.044	0.000364	0.32	0.00264	0.0035	0.00024	0.052	0.00040	279.2	2.2	281.6	2.0	305.6	12.0	99%
ker01-2	242.4	128.7	0.53	0.045	0.000394	0.35	0.0031	0.0038	0.00031	0.056	0.00041	283.1	2.4	301.6	2.3	450.0	21.3	93%
ker01-3	236.0	141.4	0.60	0.044	0.000360	0.32	0.00305	0.0034	0.00029	0.053	0.00041	280.2	2.2	283.5	2.3	322.3	18.5	98%
ker01-4	265.0	138.2	0.52	0.045	0.000357	0.32	0.00243	0.0026	0.00023	0.052	0.00034	282.1	2.2	283.6	1.9	301.9	17.6	99%
ker01-5	304.8	145.3	0.48	0.044	0.000311	0.32	0.00244	0.0033	0.00023	0.053	0.00031	279.1	1.9	282.2	1.9	309.3	13.0	98%
ker01-6	384.9	298.1	0.77	0.045	0.000306	0.33	0.00249	0.0027	0.00016	0.053	0.00031	282.6	1.9	285.9	1.9	322.3	14.8	98%
ker01-7	341.1	166.0	0.49	0.045	0.000338	0.32	0.00263	0.0040	0.00026	0.052	0.00030	282.0	2.1	283.9	2.0	298.2	17.6	99%
ker01-8	281.3	133.9	0.48	0.044	0.000321	0.31	0.0026	0.0031	0.00025	0.052	0.00033	277.9	2.0	276.9	2.0	333.4	14.8	99%
ker01-9	207.5	132.1	0.64	0.044	0.000281	0.32	0.00319	0.0023	0.00021	0.052	0.00041	278.4	1.7	279.7	2.5	287.1	-13.9	99%
ker01-10	228.2	148.9	0.65	0.044	0.000295	0.33	0.00262	0.0023	0.00019	0.054	0.00040	279.8	1.8	289.4	2.0	368.6	16.7	96%
ker01-11	186.3	131.1	0.70	0.043	0.000345	0.31	0.00325	0.0026	0.00022	0.052	0.00039	274.3	2.1	275.0	2.5	279.7	18.5	99%
ker01-12	186.5	127.4	0.68	0.044	0.000357	0.32	0.00354	0.0027	0.00023	0.052	0.00047	277.6	2.2	279.7	2.7	298.2	20.4	99%
ker01-13	198.0	128.0	0.65	0.044	0.000311	0.31	0.00297	0.0029	0.00023	0.051	0.0004	278.2	1.9	273.5	2.3	235.3	16.7	98%
ker01-14	197.4	113.2	0.57	0.042	0.000352	0.30	0.00311	0.0026	0.00021	0.052	0.00038	266.0	2.2	269.7	2.4	301.9	16.7	98%
ker01-15	310.0	147.0	0.47	0.044	0.000295	0.32	0.00228	0.0024	0.00019	0.052	0.00031	279.0	1.8	279.9	1.8	287.1	13.0	99%
ker01-16	187.1	109.2	0.58	0.044	0.000296	0.31	0.00291	0.0026	0.00022	0.052	0.00037	279.1	1.8	277.7	2.3	264.9	13.9	99%
ker01-17	423.5	265.6	0.63	0.044	0.000318	0.31	0.00236	0.0023	0.00015	0.051	0.00027	279.4	2.0	277.3	1.8	261.2	8.3	99%
ker01-18	300.4	101.3	0.34	0.044	0.000312	0.31	0.00259	0.0037	0.00028	0.051	0.00030	279.2	1.9	275.0	2.0	239.0	8.3	98%
ker01-19	190.1	113.8	0.60	0.043	0.000421	0.30	0.00375	0.0021	0.00021	0.051	0.00048	273.0	2.6	270.1	2.9	255.6	50.0	98%
ker01-20	257.3	154.9	0.60	0.043	0.000321	0.30	0.00264	0.0022	0.0002	0.051	0.00036	273.3	2.0	268.1	2.1	233.4	16.7	98%
二长花岗岩锆石U-Pb同位素分析数据
测点	w_B/(μg·g^-1)		Th/U	²⁰⁶Pb/²³⁸U		²⁰⁷Pb/²³⁵U		²⁰⁸Pb/²³²Th		²⁰⁷Pb/²⁰⁶Pb		²⁰⁶Pb/²³⁸U		²⁰⁷Pb/²³⁵U		²⁰⁷Pb/²⁰⁶Pb		谐和度
测点	U	Th	Th/U	比值	1σ	比值	1σ	比值	1σ	比值	1σ	年龄/Ma	1σ	年龄/Ma	1σ	年龄/Ma	1σ	谐和度
ker02-1	681.1	82.6	0.12	0.043	0.00032	0.31	0.00239	0.0030	0.00031	0.052	0.00025	273.4	2.0	275.1	1.8	300.1	9.3	99%
ker02-2	241.9	113.1	0.47	0.044	0.00035	0.31	0.00334	0.0031	0.00029	0.052	0.00040	275.0	2.1	277.3	2.6	294.5	21.3	99%
ker02-3	196.3	24.8	0.13	0.067	0.00109	0.51	0.00962	0.0166	0.00168	0.055	0.00036	420.4	6.6	420.8	6.5	416.7	-17.6	99%
ker02-4	122.8	32.0	0.26	0.055	0.00060	0.40	0.00459	0.0097	0.00097	0.053	0.00039	347.4	3.7	342.5	3.3	322.3	16.7	98%
ker02-5	960.7	239.4	0.25	0.044	0.00028	0.31	0.00238	0.0026	0.00020	0.052	0.00027	275.0	1.7	274.1	1.8	264.9	13.0	99%
ker02-6	613.7	114.6	0.19	0.043	0.00030	0.31	0.00244	0.0035	0.00032	0.051	0.00022	273.1	1.9	271.8	1.9	261.2	41.7	99%
ker02-7	581.1	53.3	0.09	0.044	0.00045	0.32	0.00354	0.0050	0.00054	0.052	0.00029	276.8	2.8	278.3	2.7	300.1	11.1	99%
ker02-8	7.3	3.9	0.53	0.068	0.00167	0.54	0.03039	0.1032	0.02170	0.059	0.00331	421.2	10.1	438.2	20.0	553.7	119.4	96%
ker02-9	460.0	23.0	0.05	0.044	0.00029	0.31	0.00230	0.0119	0.00148	0.052	0.00027	275.7	1.8	275.2	1.8	272.3	11.1	99%
ker02-10	143.5	68.1	0.47	0.043	0.00031	0.30	0.00360	0.0042	0.00052	0.051	0.00053	273.7	1.9	270.1	2.8	239.0	24.1	98%
ker02-11	160.2	79.0	0.49	0.043	0.00032	0.31	0.00372	0.0042	0.00045	0.052	0.00050	272.8	2.0	272.2	2.9	333.4	22.2	99%
ker02-12	654.5	20.0	0.03	0.044	0.00026	0.31	0.00241	0.0099	0.00124	0.052	0.00026	274.7	1.6	275.3	1.9	279.7	-16.7	99%
ker02-13	415.7	90.2	0.22	0.043	0.00026	0.31	0.00247	0.0041	0.00039	0.052	0.00031	271.8	1.6	273.6	1.9	300.1	13.0	99%
ker02-14	159.8	190.8	1.19	0.056	0.00042	0.42	0.00401	0.0033	0.00024	0.055	0.00047	350.1	2.5	359.6	2.9	433.4	18.5	97%
ker02-15	291.4	175.2	0.60	0.043	0.00044	0.31	0.00400	0.0029	0.00026	0.051	0.00037	274.4	2.7	272.8	3.1	257.5	14.8	99%
ker02-16	117.6	55.1	0.47	0.055	0.00051	0.41	0.00564	0.0040	0.00043	0.054	0.00053	346.7	3.1	351.5	4.0	383.4	22.2	98%
ker02-17	398.6	32.4	0.08	0.043	0.00033	0.31	0.00299	0.0074	0.00105	0.051	0.00027	274.2	2.0	272.7	2.3	257.5	38.9	99%
ker02-18	211.8	80.6	0.38	0.055	0.00043	0.40	0.00403	0.0044	0.00045	0.054	0.00037	343.9	2.6	344.9	2.9	350.1	10.2	99%
ker02-19	179.1	85.7	0.48	0.055	0.00045	0.41	0.00357	0.0047	0.00045	0.054	0.00037	346.8	2.8	351.1	2.6	383.4	14.8	98%
ker02-20	345.3	137.4	0.40	0.056	0.00044	0.42	0.00319	0.0034	0.00033	0.055	0.00032	348.2	2.7	357.0	2.3	416.7	-17.6	97%

下载: 导出CSV

表 2 矿床硫同位素组成结果

Table 2. The isotopic component for sulfur in deposit

样品编号	矿物名称	δ³⁴S_V-CDT/‰
Ker 14	黄铁矿	-7.2
Ker 15	黄铁矿	-3.9
Ker 20	黄铁矿	-2.9
Ker 21	黄铁矿	-0.6
Ker 22	黄铁矿	0.1
Ker 23	黄铁矿	-0.5
Ker 24	黄铁矿	-1.8
Ker 25	黄铁矿	0.3
Ker 26	黄铁矿	-2.4
Ker 27	黄铁矿	-2.5
Ker 34	黄铁矿	-1.4
Ker 35	黄铁矿	0.3
Ker 36	黄铁矿	0.7
Ker 40	黄铁矿	0.1
Ker 41	黄铁矿	-1.7

下载: 导出CSV

参考文献(28)

[1]	赵一鸣.中国铁矿资源现状、保证程度和对策[J].地质论评, 2004, 50(4): 396-417. http://www.cnki.com.cn/Article/CJFDTOTAL-DZLP200404010.htm
[2]	张泾生.我国铁矿资源开发利用现状及发展趋势[J].钢铁, 2007, 42(2): 1-6. doi: 10.7513/j.issn.1004-7638.2007.02.001
[3]	焦玉书,周伟.世界铁矿资源开发利用和我国进口铁矿石的发展态势(续) [J].中国冶金, 2004, 85(12): 15-18. doi: 10.3969/j.issn.1006-9356.2004.12.004
[4]	何国琦, 成守德, 徐新, 李锦轶, 郝杰.中国新疆及邻区大地构造图(1∶2500000)说明书[M].北京:地质出版社, 2004: 1-65.
[5]	侯可军,李延河,田有荣.LA-MC-ICP-MS锆石微区原位U-Pb定年技术[J].矿床地质, 2009, 28(4): 481-492. http://www.cnki.com.cn/Article/CJFDTOTAL-KCDZ200904009.htm
[6]	Nasdala L, Hofmeister W, Norberg N, Mattinson J M, Corfu F, Dor W, Kamo S L, Kennedy A K, Kronz A, Reiners P W, Frei D, Kosler J, Wan Y, Götze J, Hager T, Kröner A, Valley J. Zircon M257—A homogeneous natural reference material for the ion microprobe U-Pb analysis of zircon [J].Geostandards and Geoanalytical Research, 2008, 32: 247-265. doi: 10.1111/ggr.2008.32.issue-3
[7]	Ludwig K R.User′s Manual for Isoplot 3.0: A Geochro-nological Toolkit for Microsoft Excel[M].Berkeley: Berkeley Geochronology Center Special Publication, 2003: 1-71.
[8]	Slama J, Kosler J, Condon D J, Crowley J L, Gerdes A, Hanchar J M, Horstwood M S A, Morris G A, Nasdala L, Norberg N, Schaltegger U, Schoene B, Tubrett M N, Whitehouse M J.Plesovice zircon—A new natural reference material for U-Pb and Hf isotopic microanalysis[J].Chemical Geology, 2008, 249: 1-35. doi: 10.1016/j.chemgeo.2007.11.005
[9]	Claesson S, Vetrin V, Bayanova T, Downes H.U-Pb zircon age from a Devonian carbonatite dyke, Kola peninsula, Russia: A record of geological evolution from the Archaean to the Palaeozoic[J].Lithos, 2000, 51(1-2): 95-108. doi: 10.1016/S0024-4937(99)00076-6
[10]	Belousova E A, Griffin W L, O′Reilly S Y, Fisher N I.Apatite as an indicator mineral for mineral exploration: Trace-element compositions and their relationship to host rock type[J].Journal of Geochemical Exploration, 2002, 76: 45-69. doi: 10.1016/S0375-6742(02)00204-2
[11]	李锦轶.试论中国新疆准噶尔山系古生代板块构造演化[M].北京: 北京科学技术出版社, 1991: 92-108.
[12]	何国琦, 李茂松, 刘德权.中国新疆古生代地壳演化及成矿[M].乌鲁木齐: 新疆人民出版社, 香港: 香港文化教育出版社, 1994: 1-437.
[13]	童英, 王涛, Kovach V P, 洪大卫, 韩宝福.阿尔泰中蒙边界塔克什肯口岸后造山富碱侵入岩体的形成时代、成因及其地壳生长意义[J].岩石学报, 2006, 22(5): 1267-1278. http://www.cnki.com.cn/Article/CJFDTOTAL-YSXB200605018.htm
[14]	刘崴国,韩静波,薛晓峰,郭伟伟.阿尔泰山南缘二叠纪地壳伸展减薄——来自侵入岩的证据[J].新疆地质, 2011, 29(3): 270-274. http://www.cnki.com.cn/Article/CJFDTOTAL-XJDI201103006.htm
[15]	韩宝福,季建清,宋彪,陈立辉,李宗怀.新疆喀拉通克和黄山东含铜镍矿镁铁-超镁铁杂岩体的SHRIMP锆石U-Pb年龄及其地质意义[J].科学通报, 2004, 49(22): 2324-2328. doi: 10.3321/j.issn:0023-074X.2004.22.012
[16]	周刚, 张招崇, 王新昆, 王祥, 罗世宾, 何斌, 张小林.新疆玛因鄂博断裂带中花岗质糜棱岩锆石U-Pb SHRIMP和黑云母⁴⁰Ar-³⁹Ar年龄及意义[J].地质学报, 2007, 81(3): 359-369.
[17]	周刚, 张招崇, 罗世宾, 何斌, 王祥, 应立娟, 赵华, 李爱红, 贺永康.新疆阿尔泰山南缘玛因鄂博高温型强过铝花岗岩年龄、地球化学特征及其地质意义[J].岩石学报, 2007, 23(8): 1909-1920. http://www.cnki.com.cn/Article/CJFDTOTAL-YSXB200708011.htm
[18]	童英, 洪大卫, 王涛, 王式洸, 韩宝福.阿尔泰造山带南缘富蕴后造山线形花岗岩体锆石U-Pb年龄及其地质意义[J].岩石矿物学杂志, 2006, 25(2): 85-89. http://www.cnki.com.cn/Article/CJFDTOTAL-YSKW200602001.htm
[19]	刘锋, 张超, 杨富全.新疆阿尔泰南缘加尔巴斯套铁矿床成矿时代及成矿作用研究[J].矿床地质, 2012,31(6): 1277-1288. http://www.cnki.com.cn/Article/CJFDTOTAL-KCDZ201206013.htm
[20]	王涛, 洪大卫, 童英, 韩宝福, 石玉若.中国阿尔泰造山带后造山喇嘛昭花岗岩体锆石SHRIMP年龄、成因及陆壳垂向生长意义[J].岩石学报, 2005, 21(3): 640-650. http://www.cnki.com.cn/Article/CJFDTOTAL-YSXB200503007.htm
[21]	李香仁, 刘锋, 杨富全.新疆阿尔泰克因布拉克铜锌矿区二云母正长花岗岩成岩时代及其地质意义探讨[J].新疆地质, 2012, 30(1):5-11. http://www.cnki.com.cn/Article/CJFDTOTAL-XJDI201201003.htm
[22]	肖序常,汤耀庆,李锦轶,赵民,冯益民,朱宝清.古中亚复合巨型缝合带南缘构造演化[M]//肖序常,汤耀庆,主编.古中亚复合巨型缝合带南缘构造演化.北京:北京科学技术出版社, 1991: l-24.
[23]	于学元, 梅厚均, 杨学昌, 王俊达.额尔齐斯火山岩及其构造演化[M]//涂光炽,主编.新疆北部固体地球科学新进展.北京:科学出版社, 1993: 185-198.
[24]	成守德, 王元龙.新疆大地构造演化基本特征[J].新疆地质, 1998, 16(2): 98-107. http://www.cnki.com.cn/Article/CJFDTOTAL-XJDI199802000.htm
[25]	李华芹,谢才富,常海亮,蔡红,朱家平,周肃.新疆北部主要有色金属矿床成矿期同位素年代学研究[M].北京:地质出版社, 1998: 202-206.
[26]	Han B F, Ji J Q, Song B, Chen L H, Li Z H.SHRIMP zircon U-Pb ages of Kalatongke No.1 and Huangshandong Cu-Ni-bearing mafic-ultramafic complexes, North Xinjiang, and geological implications [J].Chinese Science Bulletin, 2004, 49(22): 2424-2429.
[27]	Chen B, Jahn B.Genesis of post-collisional granitoids and basement nature of the Junggar Terrane, NW China: Nd-Sr isotope and trace element evidence [J].Journal of Asian Earth Sciences, 2004, 23: 691-703. doi: 10.1016/S1367-9120(03)00118-4
[28]	Chen B, Arakawa Y. Elemental and Nd-Sr isotopic geo-chemistry of granitoids from the West Junggar foldbelt (NW China), with implications for Phanerozoic continental growth[J]. Geochimica et Cosmochimica Acta, 2005, 69(5): 1307-1320. doi: 10.1016/j.gca.2004.09.019