安徽大别山地区沙坪沟超大型斑岩钼矿床成矿系统特征

doi:10.13745/j.esf.sf.2020.3.26

地学前缘 ›› 2020, Vol. 27 ›› Issue (2): 353-372.DOI: 10.13745/j.esf.sf.2020.3.26

安徽大别山地区沙坪沟超大型斑岩钼矿床成矿系统特征

任志¹^,²(), 周涛发¹^,³^,^*(), 袁峰¹^,³, 张怀东⁴

1.合肥工业大学资源与环境工程学院,安徽合肥 230009
2.东华理工大学核资源与环境国家重点实验室,江西南昌 330013
3.安徽省矿产资源与矿山环境工程技术研究中心,安徽合肥 230009
4.安徽省地质矿产勘查局313地质队,安徽六安 237271

收稿日期:2019-12-01 修回日期:2019-12-28 出版日期:2020-03-25 发布日期:2020-03-25
通讯作者: 周涛发
作者简介:任志(1989—),男,博士,讲师,矿物学、岩石学、矿床学专业。E-mail: renzhi@outlook.com
基金资助:
国家重点研发计划项目(2016YFC0600206);国家自然科学基金项目(41872081);国家自然科学基金项目(41320104003);中国地调局地质大调查项目(1212011220243);东华理工大学专项经费项目(DHBK2019315)

Characteristics of the metallogenic system of the Shapinggou super-large porphyry molybdenum deposit in the Dabie orogenic belt, Anhui Province

REN Zhi¹^,²(), ZHOU Taofa¹^,³^,^*(), YUAN Feng¹^,³, ZHANG Huaidong⁴

1. School of Resources and Environmental Engineering, Hefei University of Technology, Hefei 230009, China
2. State Key Laboratory of Nuclear Resources and Environment, East China University of Technology, Nanchang 330013, China
3. Anhui Mineral Resources and Mine Environmental Engineering Research Center, Hefei 230009, China
4. No. 313 Geological Party, Anhui Bureau of Geology and Mineral Exploration, Lu'an 237271, China

Received:2019-12-01 Revised:2019-12-28 Online:2020-03-25 Published:2020-03-25
Contact: ZHOU Taofa

摘要/Abstract

摘要：

东秦岭—大别钼成矿带斑岩钼矿床的成矿地球动力学、地球化学背景和成岩成矿机制等备受研究学者的重视,但仍有许多成矿学问题需要加强研究,特别是超大型钼矿床成矿系统的组成特征、形成与演化等还需要加以系统总结。本文以翟裕生院士的成矿系统理论为指导,选取具有代表性的沙坪沟斑岩钼矿床作为研究对象,在总结前人研究成果和作者前期工作的基础上,归纳沙坪沟钼矿床地质特征,分析成矿系统的构成,通过综合对比研究,提取系统成矿特色。沙坪沟钼矿床形成于陆内伸展环境,是中国东部中生代大规模岩浆-成矿事件的产物,其含矿斑岩起源于古老下地壳+大别杂岩+岩石圈地幔,钼主要源自古老下地壳+大别杂岩,岩浆演化与热液活动持续了约24 Ma,形成了一个直径约为3 km左右的球状巨型斑岩钼成矿系统。成矿流体经历了由早期的高温、中盐度、较高氧逸度、低碱度、低pH值、低密度,中期的中高温-中温、低盐度与高盐度共存、低密度与高密度共存、低氧逸度、富CO₂,向晚期的低温、低盐度、贫CO₂、较高氧逸度、较高碱度、较高pH值、较高密度进行演化的过程,含Cl络合物由于温度、氧逸度下降和流体沸腾产生的相分离导致Mo的沉淀,形成了巨量钼金属的聚集。与国内外主要的斑岩钼成矿系统相比,沙坪沟钼矿床的成矿系统具有单矿体、巨系统、先天富、长孕育、多来源、高演化、多期次、超富集等鲜明的成矿特色。应用成矿系统理论,不断深入研究这一世界级超大型高品位斑岩型钼矿床的成矿作用和成矿过程,对于全面揭示斑岩型钼矿床的成因以及同类矿床的找寻都具有十分重要的意义。

关键词: 成矿系统, 成矿特色, 矿床地质特征, 斑岩钼矿床, 沙坪沟, 大别山地区

Abstract:

The ore-forming geodynamics, geochemical background, diagenesis, and mineralization mechanism of the porphyry molybdenum deposit in the East Qinling-Dabie molybdenum metallogenic belt have attracted the attention of researchers, but some mineralization problems still need to be addressed. In particular, the composition, formation, and evolution of the ore-forming system of the super-large molybdenum deposits need to be systematically summarized. Based on the theory on metallogenic systems of academician Zhai Yusheng, this paper selects the representative Shapinggou porphyry molybdenum deposit as the research object, and summarizes its geological characteristics on the basis of previous research results and the author’s preliminary work. The composition of the ore-forming system is analyzed and the distinguishing features of the system are identified through comparative research. The Shapinggou molybdenum deposit formed in the intracontinental extensional environment and is the product of the large-scale magmatic-mineralization events of the Mesozoic in Eastern China. Its ore-bearing porphyry originated from the ancient lower crust+Dabie complex+lithospheric mantle.Molybdenum mainly originated from the ancient lower crust+Dabie complex. Magma evolution and hydrothermal activity lasted approximately 24 Ma, forming a spherical giant porphyry molybdenum ore-forming system with a diameter of approximately 3 km.Ore-forming fluids have experienced early high temperature, medium salinity, higher oxygen fugacity, low alkalinity, low pH, low density, medium-term high temperature-medium temperature, low salinity-high salinity coexistence, low density-high density coexistence, low oxygen fugacity, rich CO₂, evolution to late low temperature, low salinity, poor CO₂, higher oxygen fugacity, higher alkalinity, higher pH, and higher density, including Cl.The precipitation of Mo due to phase separation caused by temperature, oxygen fugacity, and fluid boiling resulted in the formation of a large amount of molybdenum metal. Compared with the main porphyry molybdenum ore-forming systems in China and abroad, the metallogenic system of the Shapinggou molybdenum deposit has distinctive mineralization characteristics such as a single ore body, giant system, congenital rich, long gestation, multiple sources, high evolution, multiple periods, super-enrichment, etc. Applying the theory on metallogenic systems, we will continue to study the metallogenic and ore-forming processes of this super-large, high-grade porphyry molybdenum deposit to determine the genesis of the porphyry molybdenum deposits as well as search for similar deposits, both of which are of great significance.

Key words: metallogenic system, metallogenic feature, geological characteristics of deposit, porphyry molybdenum deposit, Shapinggou, Dabie orogenic belt

中图分类号:

任志, 周涛发, 袁峰, 张怀东. 安徽大别山地区沙坪沟超大型斑岩钼矿床成矿系统特征[J]. 地学前缘, 2020, 27(2): 353-372.

REN Zhi, ZHOU Taofa, YUAN Feng, ZHANG Huaidong. Characteristics of the metallogenic system of the Shapinggou super-large porphyry molybdenum deposit in the Dabie orogenic belt, Anhui Province[J]. Earth Science Frontiers, 2020, 27(2): 353-372.

图/表 9

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岩体名称及岩性	测定对象及方法	岩体年龄/Ma	资料来源
洪家大山中粒二长花岗岩	黑云母⁴⁰Ar-³⁹Ar	136.80±1.60	[66]
洪家大山花岗斑岩	LA-ICP MS锆石U-Pb	136.10±2.20	[72]
中粗粒似斑状二长花岗岩	LA-ICP MS锆石U-Pb	133.60±1.80	[72]
二长花岗岩	LA-ICP MS锆石U-Pb	133.00±1.20	[71]
仓房中粒二长花岗岩	LA-ICP MS锆石U-Pb	136.50±1.10	[48]
中粒二长花岗岩	LA-ICP MS锆石U-Pb	128.90±2.50	[72]
洪家大山石英斑岩	LA-ICP MS锆石U-Pb	137.80±1.90	[72]
中粗粒二长花岗岩	LA-ICP MS锆石U-Pb	127.00±1.00	[72]
洪家大山细粒二长花岗岩	黑云母⁴⁰Ar-³⁹Ar	130.40±1.20	[66]
辉石岩	LA-ICP MS锆石U-Pb	135.40±1.60	[48]
角闪石岩	LA-ICP MS锆石U-Pb	132.52±0.95	[48]
含斜长辉石岩	LA-ICP MS锆石U-Pb	130.70±0.69	[48]
斜长角闪石岩	LA-ICP MS锆石U-Pb	133.70±1.70	[71]
闪长岩	LA-ICP MS锆石U-Pb	127.40±1.70	[71]
含斜长辉石岩	LA-ICP MS锆石U-Pb	128.50±1.50	[71]
洪家大山细晶闪长岩脉	角闪石⁴⁰Ar-³⁹Ar	125.40±1.00	[66]
似斑状二长闪长岩	LA-ICP MS锆石U-Pb	127.70±2.90	[72]
闪长岩	LA-ICP MS锆石U-Pb	129.16±2.70	[72]
花岗闪长岩	LA-ICP MS锆石U-Pb	129.20±1.60	[71]
花岗闪长岩	LA-ICP MS锆石U-Pb	128.70±1.60	[72]
洪家大山花岗闪长岩	LA-ICP MS锆石U-Pb	(127.40±1.50)~(127.90±1.40)	[48]
沙坪沟花岗闪长岩	LA-ICP MS锆石U-Pb	125.40±0.87	[48]
石英正长岩	LA-ICP MS锆石U-Pb	122.51±0.81	[68]
中粒石英正长岩	LA-ICP MS锆石U-Pb	121.50±1.30	[68]
正长斑岩	LA-ICP MS锆石U-Pb	120.70±1.10	[68]
石英正长斑岩	LA-ICP MS锆石U-Pb	116.10±2.20	[69]
石英正长岩	LA-ICP MS锆石U-Pb	(113.70±1.40)~(116.30±1.30)	[70]
石英正长(斑)岩	LA-ICP MS锆石U-Pb	115.90±1.30	[71]
黑云母正长岩	LA-ICP MS锆石U-Pb	115.60±1.80	[72]
石英正长岩	LA-ICP MS锆石U-Pb	111.70±1.90	[67]
石英正长岩	LA-ICP MS锆石U-Pb	117.20±0.81	[48]
石英正长斑岩	LA-ICP MS锆石U-Pb	(113.25±0.41)~(114.54±0.39)	[48]
盖井隐爆角砾岩	LA-ICP MS锆石U-Pb	(113.80±1.60)~(131.70±3.20)	[73]
爆破角砾岩(基质)	LA-ICP MS锆石U-Pb	112.90±1.20	[69]
花岗斑岩	LA-ICP MS锆石U-Pb	(110.00±1.30)~(112.60 ±1.90)	[70]
花岗斑岩	LA-ICP MS锆石U-Pb	109.30±1.60	[71]
花岗斑岩	LA-ICP MS锆石U-Pb	(115.60±1.80)~(116.30±2.10)	[73]
花岗斑岩	LA-ICP MS锆石U-Pb	111.50±1.50	[67]
花岗斑岩	LA-ICP MS锆石U-Pb	(112.30±0.69)~(113.00±0.74)	[48]
闪长玢岩	LA-ICP MS锆石U-Pb	111.89±0.31	[48]

岩体名称及岩性	测定对象及方法	岩体年龄/Ma	资料来源
洪家大山中粒二长花岗岩	黑云母⁴⁰Ar-³⁹Ar	136.80±1.60	[66]
洪家大山花岗斑岩	LA-ICP MS锆石U-Pb	136.10±2.20	[72]
中粗粒似斑状二长花岗岩	LA-ICP MS锆石U-Pb	133.60±1.80	[72]
二长花岗岩	LA-ICP MS锆石U-Pb	133.00±1.20	[71]
仓房中粒二长花岗岩	LA-ICP MS锆石U-Pb	136.50±1.10	[48]
中粒二长花岗岩	LA-ICP MS锆石U-Pb	128.90±2.50	[72]
洪家大山石英斑岩	LA-ICP MS锆石U-Pb	137.80±1.90	[72]
中粗粒二长花岗岩	LA-ICP MS锆石U-Pb	127.00±1.00	[72]
洪家大山细粒二长花岗岩	黑云母⁴⁰Ar-³⁹Ar	130.40±1.20	[66]
辉石岩	LA-ICP MS锆石U-Pb	135.40±1.60	[48]
角闪石岩	LA-ICP MS锆石U-Pb	132.52±0.95	[48]
含斜长辉石岩	LA-ICP MS锆石U-Pb	130.70±0.69	[48]
斜长角闪石岩	LA-ICP MS锆石U-Pb	133.70±1.70	[71]
闪长岩	LA-ICP MS锆石U-Pb	127.40±1.70	[71]
含斜长辉石岩	LA-ICP MS锆石U-Pb	128.50±1.50	[71]
洪家大山细晶闪长岩脉	角闪石⁴⁰Ar-³⁹Ar	125.40±1.00	[66]
似斑状二长闪长岩	LA-ICP MS锆石U-Pb	127.70±2.90	[72]
闪长岩	LA-ICP MS锆石U-Pb	129.16±2.70	[72]
花岗闪长岩	LA-ICP MS锆石U-Pb	129.20±1.60	[71]
花岗闪长岩	LA-ICP MS锆石U-Pb	128.70±1.60	[72]
洪家大山花岗闪长岩	LA-ICP MS锆石U-Pb	(127.40±1.50)~(127.90±1.40)	[48]
沙坪沟花岗闪长岩	LA-ICP MS锆石U-Pb	125.40±0.87	[48]
石英正长岩	LA-ICP MS锆石U-Pb	122.51±0.81	[68]
中粒石英正长岩	LA-ICP MS锆石U-Pb	121.50±1.30	[68]
正长斑岩	LA-ICP MS锆石U-Pb	120.70±1.10	[68]
石英正长斑岩	LA-ICP MS锆石U-Pb	116.10±2.20	[69]
石英正长岩	LA-ICP MS锆石U-Pb	(113.70±1.40)~(116.30±1.30)	[70]
石英正长(斑)岩	LA-ICP MS锆石U-Pb	115.90±1.30	[71]
黑云母正长岩	LA-ICP MS锆石U-Pb	115.60±1.80	[72]
石英正长岩	LA-ICP MS锆石U-Pb	111.70±1.90	[67]
石英正长岩	LA-ICP MS锆石U-Pb	117.20±0.81	[48]
石英正长斑岩	LA-ICP MS锆石U-Pb	(113.25±0.41)~(114.54±0.39)	[48]
盖井隐爆角砾岩	LA-ICP MS锆石U-Pb	(113.80±1.60)~(131.70±3.20)	[73]
爆破角砾岩(基质)	LA-ICP MS锆石U-Pb	112.90±1.20	[69]
花岗斑岩	LA-ICP MS锆石U-Pb	(110.00±1.30)~(112.60 ±1.90)	[70]
花岗斑岩	LA-ICP MS锆石U-Pb	109.30±1.60	[71]
花岗斑岩	LA-ICP MS锆石U-Pb	(115.60±1.80)~(116.30±2.10)	[73]
花岗斑岩	LA-ICP MS锆石U-Pb	111.50±1.50	[67]
花岗斑岩	LA-ICP MS锆石U-Pb	(112.30±0.69)~(113.00±0.74)	[48]
闪长玢岩	LA-ICP MS锆石U-Pb	111.89±0.31	[48]

矿床类型		矿石品位		与成矿相关岩浆岩		矿体位置			同成因基性岩		产出位置		构造背景
Climax型钼矿床		常>0.15%		高钾钙碱性、准铝质-过铝质A型花岗岩(SiO₂含量>75%)		斑岩体内及其与围岩接触带中			普遍		裂谷或弧后盆地		弧后伸展或裂谷
Endako型钼矿床		<0.15%		高度演化I型石英二长岩(准铝质;通常SiO₂含量<70%)		斑岩体内及其与围岩接触带中			无		陆缘弧		大陆边缘挤压
沙坪沟钼矿床		平均0.14%		高钾钙碱性、准铝质-弱过铝质A型花岗岩(SiO₂含量约77%)		斑岩体内及其与围岩接触带中			有		陆陆碰撞带		板内伸展
矿床类型	岩浆源区		w(Rb)/10^-6		w(Nb)/10^-6		w(Sr)/10^-6	w(TiO₂)		K₂O/Na₂O		参考文献
Climax型钼矿床	大陆地壳±岩石圈地幔		200~800		25~200		<12	<0.2%		>1		[107-108]
Endako型钼矿床	洋壳、弧地壳、富集地幔		100~350		< 20		>100	常>0.2%		<1		[107-108]
沙坪沟钼矿床	大陆地壳+岩石圈地幔		301~483		69~163		16~64	约0.1%		>1		[12,47]

矿床类型		矿石品位		与成矿相关岩浆岩		矿体位置			同成因基性岩		产出位置		构造背景
Climax型钼矿床		常>0.15%		高钾钙碱性、准铝质-过铝质A型花岗岩(SiO₂含量>75%)		斑岩体内及其与围岩接触带中			普遍		裂谷或弧后盆地		弧后伸展或裂谷
Endako型钼矿床		<0.15%		高度演化I型石英二长岩(准铝质;通常SiO₂含量<70%)		斑岩体内及其与围岩接触带中			无		陆缘弧		大陆边缘挤压
沙坪沟钼矿床		平均0.14%		高钾钙碱性、准铝质-弱过铝质A型花岗岩(SiO₂含量约77%)		斑岩体内及其与围岩接触带中			有		陆陆碰撞带		板内伸展
矿床类型	岩浆源区		w(Rb)/10^-6		w(Nb)/10^-6		w(Sr)/10^-6	w(TiO₂)		K₂O/Na₂O		参考文献
Climax型钼矿床	大陆地壳±岩石圈地幔		200~800		25~200		<12	<0.2%		>1		[107-108]
Endako型钼矿床	洋壳、弧地壳、富集地幔		100~350		< 20		>100	常>0.2%		<1		[107-108]
沙坪沟钼矿床	大陆地壳+岩石圈地幔		301~483		69~163		16~64	约0.1%		>1		[12,47]

矿床	成矿区带	构造背景		成矿时代/Ma		金属量与平均品位	成矿岩体		赋矿围岩		围岩蚀变		与钼矿化有关的蚀变		源区特征及 Mo来源		矿化类型			矿石矿物		角砾岩			含氟矿物	参考文献
沙坪沟	大别山	下地壳拆沉后的板内伸展环境		(113.90±1.70)~ (111.10±1.20)		2.46 Mt@ 0.140%	花岗斑岩		正长岩、二长花岗岩等		石英内核、钾硅酸盐化、硅化、绢英岩化、青磐岩化、泥化等		硅化,次为钾硅酸盐化和绢英岩化		古老下地壳+大别杂岩+岩石圈地幔;古老地壳(含大别杂岩)		网脉状、脉状、细脉浸染状矿石;以石英-辉钼矿脉为主,少量石英-辉钼矿-黄铁矿脉、石英-绢云母-辉钼矿脉、辉钼矿±石英脉等			辉钼矿、黄铁矿,少量方铅矿、闪锌矿、磁铁矿、赤铁矿等		发育			萤石	[5,48]
金堆城	东秦岭	由挤压向伸展转换的环境		138.40±0.50		0.98 Mt@ 0.099%	花岗斑岩		熊耳群火山岩,高山河组石英岩、板岩		钾硅酸盐化、硅化、绢云母—黄铁矿化和青磐岩化		绢英岩化和硅化,次为钾硅酸盐化		古老下地壳;同岩浆源		以脉状、网脉状辉钼矿矿化及纹层状石英-辉钼矿脉为主,少量微细辉钼矿脉状矿化			辉钼矿、黄铁矿,少量黄铜矿、磁铁矿、闪锌矿、方铅矿		无			萤石	[11,32]
沙让	冈底斯	大陆碰撞挤压环境		51.00±1.00		0.06 Mt@ 0.061%	花岗斑岩		沉积变质杂岩		钾硅酸盐化、绢英岩化、硅化、黏土化和青磐岩化		绢英岩化,次为钾硅酸盐化		古老地壳;同岩浆源		以脉状、网脉状辉钼矿矿化及纹层状石英-辉钼矿脉为主,少量浸染状			辉钼矿、黄铁矿,少量黄铜矿、磁铁矿、闪锌矿、白钨矿		发育			无或微量	[116-117]
岔路口	大兴安岭	蒙古—鄂霍茨克洋闭合碰撞后挤压向伸展转换		145.70±1.50		1.78 Mt@ 0.087%	细晶斑岩、花岗斑岩		细晶斑岩、花岗斑岩、早奥陶世变火山岩		石英内核、硅化、钾化、绢云母化、萤石化和磁铁矿化		硅化和钾化		新生下地壳;富集岩石圈地幔		网脉状、细脉浸染状、脉状			辉钼矿、黄铁矿、方铅矿、闪锌矿、磁铁矿,少量黄铜矿		发育			萤石	[118]
曹四夭	华北板块北缘	蒙古—鄂霍茨克洋闭合碰撞后挤压向伸展转换		149~146		1.75 Mt@ 0.078%	正长花岗斑岩		石榴斜长浅粒岩和黑云石榴斜长片麻岩		硅化、钾化、绢英岩化、青磐岩化、萤石化、方柱石化、碳酸盐化、泥化		硅化和绢云母化		下地壳;同岩浆源		细脉浸染状和浸染状			辉钼矿和黄铁矿, 其次为磁铁矿、黄铜矿、磁黄铁矿, 另有少量黑钨矿		无			萤石	[119]
鹿鸣	吉黑	太平洋板块俯冲体制下挤压向伸展转换的过程中		183~178		0.89 Mt@ 0.084%	二长花岗岩、花岗斑岩		二长花岗岩、花岗斑岩		硅化、钾化、黄铁矿化、青磐岩化、云英岩化		硅化和钾化		新生下地壳;同岩浆源		主要为浸染状,次为网脉状			辉钼矿、黄铁矿,少量黄铜矿		发育			无或微量	[120]
矿床			成矿区带		构造背景	成矿时代/Ma		金属量与平均品位		成矿岩体		赋矿围岩		围岩蚀变		与钼矿化有关的蚀变		源区特征及 Mo来源	矿化类型		矿石矿物		角砾岩	含氟矿物			参考文献
Climax			科罗拉多成矿带		Rio Grande 裂谷系统的板内伸展环境	33~24		2.58 Mt@ 0.240%		细晶斑岩、花岗斑岩		前寒武纪的Idaho Springs 组的片岩和片麻岩		钾化、绢英岩化、上下泥化、青磐岩化、脉状硅化、弥散状硅化、磁铁矿和黄玉化、云英岩化和石榴石化		钾长石化,次为绢英岩化		古老地壳;同岩浆源	脉状、细脉状和角砾状		辉钼矿、黄铁矿、黑钨矿、锡石、菱锰矿、闪锌矿、磁黄铁矿、方铅矿、磁铁矿,少量黄铜矿、钨锰矿		无	萤石、黄玉			[79,121]
Urad- Henderson			科罗拉多成矿带		Rio Grande 裂谷系统的板内伸展环境	28		1.24 Mt@ 0.171%		多期次岩钟状流纹斑岩、细晶斑岩、花岗斑岩		前寒武纪花岗岩和片麻岩		黏土化、绢云母-石英-黄铁矿化、石英-黄玉化、硅化、钾化、云英岩、萤石化和黄玉化		钾长石化、绢英岩化和黄玉化		古老地壳;同岩浆源	脉状、细脉状和角砾状		辉钼矿、黄铁矿、黑钨矿、菱锰矿、闪锌矿、磁黄铁矿、方铅矿、磁铁矿,少量黄铜矿、锡石		发育	萤石、黄玉			[79,109,122-123]
Questa			科罗拉多成矿带		Rio Grande 裂谷系统的板内伸展环境	25~24		0.44 Mt@ 0.144%		流纹斑岩、细晶斑岩、花岗斑岩		第三纪安山岩、流纹岩、凝灰岩和前寒武纪花岗岩及片麻岩		钾硅酸盐化、黑云母-绢云母化、石英-绢云母-黄铁矿-高岭石化、青磐岩化,萤石和黄玉化		绢英岩化、钾长石化			主要为热液角砾岩型矿化,常与石膏/硬石膏以及绿柱石共生,少量网脉状矿化		辉钼矿,少量黄铁矿、方铅矿、黄铜矿、白钨矿		发育	萤石			[124-125]
Endako			中加拿大科迪勒拉成矿带		Kula和 arallon板块向北美板块俯冲挤压背景	144		0.23 Mt@ 0.082%		石英二长岩		石英二长岩		钾长石化、石英-绢云母-黄铁矿化、高岭土化、碳酸盐化和少量表生蚀变		钾长石化、绢英岩化和高岭土化		俯冲板片;同岩浆源	网脉状和纹层状辉钼矿矿化,少量裂隙面矿化和浸染状矿化		辉钼矿、黄铁矿、磁铁矿,少量黄铜矿、斑铜矿、辉铋矿、白钨矿、镜铁矿、方铅矿		无	无或微量			[126-127]
Malala			北Sulawesi 岩浆带		俯冲后的晚碰撞到后碰撞环境	4.25~4.12		1 Mt@ 0.140%		正长- 二长花岗斑岩		花岗岩、花岗闪长岩		钾化、强硅化、绢云母-绿泥石-碳酸盐化和碳酸盐-粘土化		绢英岩化,次为钾化			网脉状石英-辉钼矿、脉状含辉钼矿矿矿化,少量纹层状石英-辉钼矿矿化		辉钼矿、黄铁矿,少量黄铜矿、闪锌矿、磁黄铁矿、方铅矿、磁铁矿		无	无或微量			[128]

安徽大别山地区沙坪沟超大型斑岩钼矿床成矿系统特征

Characteristics of the metallogenic system of the Shapinggou super-large porphyry molybdenum deposit in the Dabie orogenic belt, Anhui Province

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