西藏甲玛铜多金属矿床角岩岩石学与其蚀变—矿化演进序列研究
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摘要
西藏甲玛铜多金属矿床位于冈底斯-念青唐古拉地块中部,探明控制资源储量达铜当量1500多万吨。以野外第一手的精细岩心地质编录(超过3万米)为基础,采用岩、矿石光薄片显微鉴定、电子探针分析、主量元素分析、黑云母LA-ICP-MS微量元素原位微区分析、黑云母红外光谱分析,开展岩石学、矿石学和岩石地球化学分析研究,查明了212个钻孔角岩的厚度、Cu、Mo、Au、Ag、 Pb、Zn的元素含量,进行了角岩岩石学和角岩蚀变一矿化演进序列的研究。
研究表明,角岩岩石类型划分为成矿前角岩与成矿期角岩,多属钠长绿帘角岩相,矿物共生组合主要为钠长石+黑云母+石英。成矿前角岩以细晶化为主要特征,大多没有出现独立晶形的结晶矿物,其岩性主要为原生黑云母角岩(具典型斑点状、条带状构造)、长英质角岩；成矿期角岩以含有独立晶形的热液结晶矿物为特征,其岩性主要为硅化角岩、热液黑云母-绿泥石角岩等。参照地层接触关系、岩石组构特征,通过岩石化学和地球化学特征进行综合对比,确定了角岩的原岩为林布宗组砂板岩和碳质板岩。
通过0-40勘探线各钻孔角岩与角岩型矿体厚度等值线图,与各钻孔角岩内Cu、Mo元素丰度浓集中心综合对比,以及最新的地质勘探发现,对隐伏斑岩岩体进行了定位预测。
角岩中黑云母按其产状可区分为原生黑云母和热液黑云母,原生黑云母和热液黑云母的含铜性存在显著的差异,原生黑云母基本不含铜,热液黑云母则普遍含有Cu,表现出Cu元素的富集,而Mo元素在原生黑云母和热液黑云母中普遍存在,并不具有选择性赋存的特征。角岩中的热液黑云母根据蚀变矿物共生组合与蚀变产状可以分为A类、B类、C类和D类：A类黑云母产出于石英脉中,矿物共生组合为石英+黑云母(Q+Bi)；B类黑云母产出于石英脉中,矿物共生组合为石英+黑云母+绿泥石(Q+Bi+Chl);C类黑云母产出于石英脉中,矿物共生组合为石英+黑云母+高岭石(Q+Bi+Kln);D类黑云母产出于面型的热液黑云母—伴生绿泥石化蚀变中,矿物伴生组合为黑云母—绿泥石(Bi-Chl),指示钾化蚀变或退变质型钾化蚀变。A类、C类、D类黑云母可较好指示角岩型Cu矿化,四类角岩热液黑云母的原位微区Cu、Pb、Zn元素含量与相应孔深岩矿石Cu、Pb、Zn元素含量呈现正相关关系。
角岩内发育的蚀变和矿化空间演进具有如下规律,从下到上呈现了面型钾化+黄铜矿矿化→退变质型钾化+黄铜矿化→面型绿泥石化+含绿泥石石英脉+黄铜矿化→脉状硅化(石英+黄铜矿→石英+黄铜矿+辉钼矿→石英+辉钼矿)；成矿时间上从早到晚表现为,早期大规模的富酸性全岩浸透性硅质热液交代作用(引起自组织结构)伴随黄铁矿化→钾硅酸盐矿物黑云母的大量形成伴随黄铜矿化、黄铁矿化→钾硅酸盐矿物的水解退化变质伴随黄铜矿化、黄铁矿化→热液绿泥石蚀变大量形成伴随黄铜矿化、黄铁矿化→局部团斑状硅化作用伴随黄铜矿化→脉状硅化作用,形成石英+黄铜矿→石英+黄铜矿+辉钼矿→石英+辉钼矿。早期形成的辉钼矿形成于石英脉脉壁,中晚期的形成的辉钼矿赋存于石英脉中,晚期形成的辉钼矿生长于石英脉脉中的晶洞构造中；在任一阶段矿化演化过程中,辉钼矿总是首先以微细稀疏浸染状产出,随后以连续稠密浸染状产出,最后以片状自形晶产出。
精细岩心地质编录成果显示,通过单块岩心手标本,可以清晰的识别出角岩或角岩型矿石从面型蚀变到脉型蚀变,从蚀变矿物共(伴)生组合到矿物产出状态,判别出各类脉体的穿插关系及其形成的时间先后,进而可以指示蚀变类型、矿化物质组成及其组构演进序列。
综上所述,通过对甲玛铜多金属矿床角岩与角岩型矿化特征及演化的研究,解决了甲玛铜多金属矿床角岩岩石类型与成因意义、黑云母含矿性及其成矿指示、角岩蚀变—矿化演进序列问题,预测了深部隐伏的含矿斑岩体,同时解释了甲玛矿床角岩型矿体形成了巨量金属富集的成因。
The Jiama Copper polymetallic deposit is located in the central part of the Gangdese-Nyainqentanglha terrane. Metal resources of EQCu exceeds14,000,000t. This study has discussed on the petrology and alteration-mineralization evolution rhythm of hornfels based on the basic geological mapping, core logging, thin section description and microanalyses and also combined with electron microprobe analysis, major elements analysis, trace element LA-ICP-MS in situ analysis of biotite, infrared spectrography analysis of biotite and contouring of hornfels thickness and Cu, Mo, Au, Ag, Pb, Zn mineralization element content formed in them by212drilling holes.
Research shows that the hornfels thermal metamorphism is well developed in Jiama polymetallic copper deposit. Rock types of hornfels can be divided into the pre-oreforming hornfels and the syn-oreforming ones, belonging to AEH Face with the main mineral paragenetic association—albite+biotite+quartz. The pre-oreforming hornfels consist of protogenic biotite hornfels with typical mottled and banded structure, and felsic hornfels, characterized by refining-grain, most phenocryst mineral without independent morphology. The syn-oreforming hornfels include silicified hornfels and hydrothermal biotite-chlorite hornfels, characte-rized by phenocryst mineral formed in good crystal habit. Based on the stratum contact relationship and the rock fabric, protoliths of hornfels are inferred as sandy slates and carbonaceous slates by comparision for features of petrochemistry and geochemistry.
On condition that hornfels are natural trace material for thermal metamorphism, the author contours the thickness of hornfels and mineralization formed in them, and contours the concentration center of abundance of Cu and Mo, which helps to indicate the location of the concealed porphyry with the latest exploration results.
The biotite from hornfels can be distinguished into protogenic and hydrothermal biotite.. Compared with protogenic biotite, there is more Cu enriched in hydrothermal biotite. But Mo spread in two sorts of biotite diffusely, and don't have characteristic of selective occurrence. Hydrothermal biotite from hornfels can be divided into A, B, C and D type according paragenetic association of alteration minerals and alteration attitude. A type hornfels hydrothermal biotite occurs in quartz vein with the main alteration mineral paragenetic association quartz+biotite (Q+Bi), B type biotite in quartz vein with main alteration mineral paragenetic association quartz+biotite+chlorite (Q+Bi+Chl), C type biotite in quartz vein with main alteration mineral paragenetic association quartz+biotite+kaolinite (Q+Bi+Kin), and D type biotite grows in surface hydrothermal biotite-chlorite alteration with alteration mineral accompanying combination biotite-hlorite (Bi-Chl) indicating potassic alteration or retrometamorphism-potassic alteration. A, C and D type hornfels hydrothermal biotite can indicate Cu mineralization in hornfels well. The Cu, Pb and Zn contents from rocks have positive correlation with that in hornfels hydrothermal biotite.
Alteration-mineralization evolution rhythm of hornfels shows surface potassic alteration with chalcopyrite mineralization→retrometamorphism potassic alteration with chalcopyrite mineralization→surface chloritization+chlorite in quartz vein with chalcopyrite mineralization→nervation silicification (quartz+chalcopyrite→quartz+chalcopyrite+molybdenite→quartz+molybdenite) from the bottom up in space; and early stage large-scale rich acid siliceous hydrothermal solution total-rock metasomatic metamorphism (giving rise to good self-organization construction) with pyrite→teeming of potassium-rich silicate mineral biotite with chalcopyrite and pyrite forming→hydrolyzation retrometamorphism of potassium-rich silicate mineral with chalcopyrite and pyrite forming→teeming of hydrothermal chloritization with chalcopyrite and pyrite→partial crumb silication with chalcopyrite→nervation silication (quartz+chalcopyrite→quartz+chalcopyrite+molybdenite→quartz+molybdenite) from early to late. The early molybdenite grows along vein wall of quartz vein, and the later one occurs in the centre of quartz vein, and molybdenite in the end appears in the miarolitic structure of quartz vein. In any stage, molybdenite always displays dissemination formation in the early, then becomes successive dense dissemination, and changes into schistose texture self-structured crystal in the end.
The meticulous core logging shows single core hand specimen indicates information from surface alteration to nervation alteration, from alteration mineral paragenetic association or accompanying combination to occurence state, by which can help to distinguish intercalated relationship and formation order of all kinds of veins, and further indicate alteration-mineralization evolution rhythm of hornfels.
The study on Petrology and alteration-mineralization evolution rhythm of hornfels in Jiama deposit has solved problems as rock types and genesis significance of hornfels, ore-bearing potential of biotites and their mineralization signatures, and alteration-mineralization evolution rhythm of hornfels, which help to indicate the location of the concealed porphyry, and to explain genesis of accumulation of massive amount mineralization element in hornfels-type orebody.
研究表明,角岩岩石类型划分为成矿前角岩与成矿期角岩,多属钠长绿帘角岩相,矿物共生组合主要为钠长石+黑云母+石英。成矿前角岩以细晶化为主要特征,大多没有出现独立晶形的结晶矿物,其岩性主要为原生黑云母角岩(具典型斑点状、条带状构造)、长英质角岩；成矿期角岩以含有独立晶形的热液结晶矿物为特征,其岩性主要为硅化角岩、热液黑云母-绿泥石角岩等。参照地层接触关系、岩石组构特征,通过岩石化学和地球化学特征进行综合对比,确定了角岩的原岩为林布宗组砂板岩和碳质板岩。
通过0-40勘探线各钻孔角岩与角岩型矿体厚度等值线图,与各钻孔角岩内Cu、Mo元素丰度浓集中心综合对比,以及最新的地质勘探发现,对隐伏斑岩岩体进行了定位预测。
角岩中黑云母按其产状可区分为原生黑云母和热液黑云母,原生黑云母和热液黑云母的含铜性存在显著的差异,原生黑云母基本不含铜,热液黑云母则普遍含有Cu,表现出Cu元素的富集,而Mo元素在原生黑云母和热液黑云母中普遍存在,并不具有选择性赋存的特征。角岩中的热液黑云母根据蚀变矿物共生组合与蚀变产状可以分为A类、B类、C类和D类：A类黑云母产出于石英脉中,矿物共生组合为石英+黑云母(Q+Bi)；B类黑云母产出于石英脉中,矿物共生组合为石英+黑云母+绿泥石(Q+Bi+Chl);C类黑云母产出于石英脉中,矿物共生组合为石英+黑云母+高岭石(Q+Bi+Kln);D类黑云母产出于面型的热液黑云母—伴生绿泥石化蚀变中,矿物伴生组合为黑云母—绿泥石(Bi-Chl),指示钾化蚀变或退变质型钾化蚀变。A类、C类、D类黑云母可较好指示角岩型Cu矿化,四类角岩热液黑云母的原位微区Cu、Pb、Zn元素含量与相应孔深岩矿石Cu、Pb、Zn元素含量呈现正相关关系。
角岩内发育的蚀变和矿化空间演进具有如下规律,从下到上呈现了面型钾化+黄铜矿矿化→退变质型钾化+黄铜矿化→面型绿泥石化+含绿泥石石英脉+黄铜矿化→脉状硅化(石英+黄铜矿→石英+黄铜矿+辉钼矿→石英+辉钼矿)；成矿时间上从早到晚表现为,早期大规模的富酸性全岩浸透性硅质热液交代作用(引起自组织结构)伴随黄铁矿化→钾硅酸盐矿物黑云母的大量形成伴随黄铜矿化、黄铁矿化→钾硅酸盐矿物的水解退化变质伴随黄铜矿化、黄铁矿化→热液绿泥石蚀变大量形成伴随黄铜矿化、黄铁矿化→局部团斑状硅化作用伴随黄铜矿化→脉状硅化作用,形成石英+黄铜矿→石英+黄铜矿+辉钼矿→石英+辉钼矿。早期形成的辉钼矿形成于石英脉脉壁,中晚期的形成的辉钼矿赋存于石英脉中,晚期形成的辉钼矿生长于石英脉脉中的晶洞构造中；在任一阶段矿化演化过程中,辉钼矿总是首先以微细稀疏浸染状产出,随后以连续稠密浸染状产出,最后以片状自形晶产出。
精细岩心地质编录成果显示,通过单块岩心手标本,可以清晰的识别出角岩或角岩型矿石从面型蚀变到脉型蚀变,从蚀变矿物共(伴)生组合到矿物产出状态,判别出各类脉体的穿插关系及其形成的时间先后,进而可以指示蚀变类型、矿化物质组成及其组构演进序列。
综上所述,通过对甲玛铜多金属矿床角岩与角岩型矿化特征及演化的研究,解决了甲玛铜多金属矿床角岩岩石类型与成因意义、黑云母含矿性及其成矿指示、角岩蚀变—矿化演进序列问题,预测了深部隐伏的含矿斑岩体,同时解释了甲玛矿床角岩型矿体形成了巨量金属富集的成因。
The Jiama Copper polymetallic deposit is located in the central part of the Gangdese-Nyainqentanglha terrane. Metal resources of EQCu exceeds14,000,000t. This study has discussed on the petrology and alteration-mineralization evolution rhythm of hornfels based on the basic geological mapping, core logging, thin section description and microanalyses and also combined with electron microprobe analysis, major elements analysis, trace element LA-ICP-MS in situ analysis of biotite, infrared spectrography analysis of biotite and contouring of hornfels thickness and Cu, Mo, Au, Ag, Pb, Zn mineralization element content formed in them by212drilling holes.
Research shows that the hornfels thermal metamorphism is well developed in Jiama polymetallic copper deposit. Rock types of hornfels can be divided into the pre-oreforming hornfels and the syn-oreforming ones, belonging to AEH Face with the main mineral paragenetic association—albite+biotite+quartz. The pre-oreforming hornfels consist of protogenic biotite hornfels with typical mottled and banded structure, and felsic hornfels, characterized by refining-grain, most phenocryst mineral without independent morphology. The syn-oreforming hornfels include silicified hornfels and hydrothermal biotite-chlorite hornfels, characte-rized by phenocryst mineral formed in good crystal habit. Based on the stratum contact relationship and the rock fabric, protoliths of hornfels are inferred as sandy slates and carbonaceous slates by comparision for features of petrochemistry and geochemistry.
On condition that hornfels are natural trace material for thermal metamorphism, the author contours the thickness of hornfels and mineralization formed in them, and contours the concentration center of abundance of Cu and Mo, which helps to indicate the location of the concealed porphyry with the latest exploration results.
The biotite from hornfels can be distinguished into protogenic and hydrothermal biotite.. Compared with protogenic biotite, there is more Cu enriched in hydrothermal biotite. But Mo spread in two sorts of biotite diffusely, and don't have characteristic of selective occurrence. Hydrothermal biotite from hornfels can be divided into A, B, C and D type according paragenetic association of alteration minerals and alteration attitude. A type hornfels hydrothermal biotite occurs in quartz vein with the main alteration mineral paragenetic association quartz+biotite (Q+Bi), B type biotite in quartz vein with main alteration mineral paragenetic association quartz+biotite+chlorite (Q+Bi+Chl), C type biotite in quartz vein with main alteration mineral paragenetic association quartz+biotite+kaolinite (Q+Bi+Kin), and D type biotite grows in surface hydrothermal biotite-chlorite alteration with alteration mineral accompanying combination biotite-hlorite (Bi-Chl) indicating potassic alteration or retrometamorphism-potassic alteration. A, C and D type hornfels hydrothermal biotite can indicate Cu mineralization in hornfels well. The Cu, Pb and Zn contents from rocks have positive correlation with that in hornfels hydrothermal biotite.
Alteration-mineralization evolution rhythm of hornfels shows surface potassic alteration with chalcopyrite mineralization→retrometamorphism potassic alteration with chalcopyrite mineralization→surface chloritization+chlorite in quartz vein with chalcopyrite mineralization→nervation silicification (quartz+chalcopyrite→quartz+chalcopyrite+molybdenite→quartz+molybdenite) from the bottom up in space; and early stage large-scale rich acid siliceous hydrothermal solution total-rock metasomatic metamorphism (giving rise to good self-organization construction) with pyrite→teeming of potassium-rich silicate mineral biotite with chalcopyrite and pyrite forming→hydrolyzation retrometamorphism of potassium-rich silicate mineral with chalcopyrite and pyrite forming→teeming of hydrothermal chloritization with chalcopyrite and pyrite→partial crumb silication with chalcopyrite→nervation silication (quartz+chalcopyrite→quartz+chalcopyrite+molybdenite→quartz+molybdenite) from early to late. The early molybdenite grows along vein wall of quartz vein, and the later one occurs in the centre of quartz vein, and molybdenite in the end appears in the miarolitic structure of quartz vein. In any stage, molybdenite always displays dissemination formation in the early, then becomes successive dense dissemination, and changes into schistose texture self-structured crystal in the end.
The meticulous core logging shows single core hand specimen indicates information from surface alteration to nervation alteration, from alteration mineral paragenetic association or accompanying combination to occurence state, by which can help to distinguish intercalated relationship and formation order of all kinds of veins, and further indicate alteration-mineralization evolution rhythm of hornfels.
The study on Petrology and alteration-mineralization evolution rhythm of hornfels in Jiama deposit has solved problems as rock types and genesis significance of hornfels, ore-bearing potential of biotites and their mineralization signatures, and alteration-mineralization evolution rhythm of hornfels, which help to indicate the location of the concealed porphyry, and to explain genesis of accumulation of massive amount mineralization element in hornfels-type orebody.
引文
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