再论中国大陆斑岩Cu-Mo-Au矿床成矿作用

doi:10.13745/j.esf.sf.2020.3.8

摘要/Abstract

摘要：

本文在综述斑岩铜矿(PCDs)最新研究进展基础上,结合最新资料,重点阐释了中国大陆非弧环境PCDs的地球动力学背景、成矿岩浆起源、岩浆-流体系统演化、成矿金属(Cu,Au,Mo)和H₂O来源及富集过程。中国大型PCDs除少量产于岩浆弧外,主要产于碰撞造山环境的构造转换和地壳伸展阶段、陆内造山环境的岩石圈伸展和崩塌阶段以及活化克拉通的边缘及内部。这些非弧环境成矿斑岩多呈彼此孤立的近等间距分布的岩株或岩瘤产出,以高钾为特征,显示埃达克岩地球化学亲和性。成矿岩浆主要起源于加厚的镁铁质新生下地壳或拆沉的古老下地壳,少数起源于遭受早期俯冲板片流体/熔体交代改造过的富集地幔。大陆碰撞和陆内俯冲引起的地壳大规模增厚和紧随其后的板片撕裂、断离、岩石圈拆沉和软流圈上涌,是形成这些成矿岩浆的主要动力机制。与岩浆弧环境斑岩类似,非弧环境斑岩也相对富水(>4%H₂O)和高f(O₂)值(ΔFMQ≥+2),但H₂O不是来自俯冲板片,而是主要来自新生下地壳的角闪石分解或/和幔源富水超钾质岩浆水注入;金属Cu(Au)主要来自新生的镁铁质下地壳中含Cu硫化物的熔融分解,或者来自拆沉下地壳熔体与金属再富集的地幔岩反应,而金属Mo则主要来自具有高Mo丰度的大陆地壳。不论在岩浆弧还是非弧环境,成矿岩浆通常相对富集成矿金属(Cu,Au,Mo),但PCDs的形成并不要求成矿岩浆在初始阶段就异常富集金属组分,但要求金属硫化物相在岩浆流体出溶前没有从岩浆中饱和分离。浅成侵位的斑岩体(1~6 km)虽然可以出溶成矿流体,但大型PCDs通常要求成矿流体出溶自深部(侵位深度≥6 km)、有镁铁质岩浆持续补给的稳定大体积岩浆房。斑岩体可以分凝出不混溶的低盐度的气相和高盐度的液相,岩浆房则直接出溶出高温低盐度的富金属超临界流体。高盐度液相和低密度的超临界气相流体均可以迁移金属,伴随大规模热液蚀变,形成PCDs。

关键词: 斑岩铜矿, 成矿岩浆来源, 下地壳熔融, 水和金属来源, 富集机制, 成矿环境

Abstract:

By reviewing the latest research progress of porphyry copper deposits (PCDs) and combining with the new data, this paper focuses on discussing the geodynamic background of non-arc PCDs in Chinese mainland, the origin of ore-forming magma, the evolution of magmatic-hydrothermal system, the sources of ore-forming metals (Cu, Au, Mo) and H₂O, and their enrichment process. Except for a few PCDs formed in island arcs in China, most PCDs were formed during the stages of tectonic transformation and crustal extension in a collisional orogenic setting, and the stages of lithosphere extension and collapse, in the edge and interior of a re-activated craton. These non-arc porphyries are mostly isolated or nearly even-spaced stocks or bosses, and are characterized by high K contents and adakitic compositions. The ore-forming magmas are mainly originated from the newly formed thickened mafic crust or delaminated ancient lower crust, and a few originated from subduction fluid/melt metasomatized lithospheric mantle. Intercontinental collision and subduction led to large-scale crustal thickening, and the triggers for crustal melting include slab tearing, slab break-off, lithosphere delamination, and asthenospheric mantle upwelling. Similar to the island arc porphyries, the non-arc porphyries are also rich in water (> 4 wt% H₂O) and f(O₂) (ΔFMQ ≥+2). We think H₂O does not come from the subducting slab, but mainly from the decomposition of amphibole in the newly formed lower crust or injection of H₂O-rich ultrapotassic melt. Cu (Au) mainly comes from the decomposition of Cu-bearing sulfides in the newly formed lower mafic crust, or from the metal-rich lithospheric mantle reacted with delaminated lower crust. In contrast, Mo mainly comes from the continental crust in high Mo abundance. Regardless of island arc or non-arc settings, ore-forming magmas are generally enriched with metals (Cu, Au, Mo). Formation of PCDs does not require the incipient magma abnormally rich in metals, but requires sulfides not being saturated and separated from magma before exsolution of magmatic fluid. Although shallowly emplaced porphyry (1-6 km) can dissolve ore-forming fluids, large-scale PCDs usually require ore-forming fluids to dissolve from the deep part (emplacement depth ≥6 km) and have continuous mafic melt input. Shallowly emplaced porphyry can separate and condense immiscible low-salinity vapor phase and high-salinity liquid phase, while the deep-seated magma chamber directly dissolves high-temperature and low-salinity metal-rich supercritical fluid. Both high-salinity liquid phase and low-density supercritical vapor-phase fluid can transport metals and form PCDs with large-scale hydrothermal alteration.

Key words: porphyry copper deposit, origin of ore-forming magma, melting of lower crust, water and metal source, enrichment mechanism, metallogenic setting

中图分类号:

侯增谦, 杨志明, 王瑞, 郑远川. 再论中国大陆斑岩Cu-Mo-Au矿床成矿作用[J]. 地学前缘, 2020, 27(2): 20-44.

HOU Zengqian, YANG Zhiming, WANG Rui, ZHENG Yuanchuan. Further discussion on porphyry Cu-Mo-Au deposit formation in Chinese mainland[J]. Earth Science Frontiers, 2020, 27(2): 20-44.

图/表 9

图1 全球范围超大型斑岩铜矿分布图(据文献[23])

Fig.1 Distribution of giant porphyry copper deposits in the world. Adapted from [23].

图2 中国大陆非弧环境斑岩型矿床分布图(中国大陆构造格架据文献[36])

Fig.2 Distribution map of non-arc porphyry deposits in Chinese mainland (tectonic framework of Chinese mainland from [36])

图3 非弧环境斑岩铜矿岩浆起源和动力学背景示意图(据文献[20]修改) a—碰撞造山带晚碰撞走滑阶段形成的PCDs。大洋板片流体交代的楔形地幔和弧岩浆底侵形成的新生下地壳在碰撞期发生部分熔融,分别形成含Au-Cu和Cu-Mo岩浆,其侵位受大规模走滑断裂活动控制。b—碰撞造山后碰撞地壳伸展阶段形成的PCDs。碰撞前的弧岩浆在地壳底部底侵形成新生下地壳(含硫化物和含水堆积带),其部分熔融和硫化物分解形成含Cu-Mo岩浆,其侵位受横切碰撞带的正断层系统控制。c—陆内造山岩石圈伸展阶段形成的PCDs。经历强烈陆内俯冲和地壳加厚后的岩石圈因软流圈上涌而伸展,诱发新生的镁铁质下地壳熔融,产生富Cu-Au岩浆。d—陆内造山带崩塌阶段形成的PCDs。岩石圈拆沉导致下地壳熔融,其熔体与上覆的交代富集的地幔岩发生反应,产生富Cu-Fe-Au岩浆。

Fig.3 Schematic diagram of magma origin and dynamic background for non-arc porphyry-type copper deposits. Modified from [20].

图4 西藏成矿斑岩岩浆H2O含量(a)与超钾质岩浆注水模式(b) a—根据实验相平衡实验资料以及斑岩锆石Ti温度和Zr含量,估计斑岩岩浆水含量约11%[175];b—模式强调,来自交代地幔的富水超钾质岩浆注入下地壳,诱发注水熔融产生富水岩浆,这些岩浆注入浅位岩浆房,将向斑岩岩浆系统提供额外的水[129]。

Fig.4 H2O contents of metallogenic porphyry magma (a) and water injection model of ultrapotash magma (b) in Tibet

图5 成矿斑岩系统金属Cu来源的几种可能模式 a—来自大洋俯冲板片的流体携带金属Cu(Au)交代岩石圈地幔(SCLM),后者熔融产生富Cu(Au)斑岩岩浆[15]。b—来自流体交代富集地幔的弧岩浆在加厚地壳底部沉淀含Cu硫化物,使下地壳初始富集Cu。随后上侵的弧岩浆活化并利用这些金属,形成大型PCDs[209]。c—大陆碰撞前,幔源弧岩浆在加厚地壳底部大规模底侵和堆积,形成含Cu新生下地壳;碰撞期新生下地壳熔融产生富Cu斑岩岩浆[22,106,210]。d—拆沉下地壳熔融产生的熔体与金属再富集的岩石圈地幔反应,并从中萃取金属Cu(Au),形成含矿斑岩岩浆[6]。

Fig.5 Possible models for origin of metallic Cu in metallogenic porphyry system

图6 西藏冈底斯带俯冲型斑岩与碰撞型斑岩锆石Hf同位素组成反映金属Cu在下地壳的亏损与富集(据文献[106,221])

Fig.6 Hf isotopic composition of zircon from subduction-related (Jurassic) and collision-related (Miocene) porphyry in Gangdese, Tibet, reflecting enrichment or depletion of Cu in the Tibetan lower crust. Adapted from [106,221].

图7 斑岩岩浆-成矿系统的结构[233]与岩浆流体出溶记录 a—形成斑岩铜矿通常要求:(1)源于地幔的超钾镁铁质岩浆注入,提供岩浆水,并维持斑岩岩浆房的稳定发育和结晶分异,(2)侵位于6 km深处的岩浆房,并发生水饱和和流体出溶,(3)成矿流体向上运移和排泄,与围岩发生水岩反应,形成斑岩成矿系统;b—记录岩浆房流体出溶过程的单项固结结构石英(伊朗NowChun成矿斑岩的UST石英、西藏驱龙铜矿的UST石英、河南夜长坪斑岩钼矿的UST)。

Fig.7 Architecture of porphyry magma metallogenic system (adapted from [233]) and records for exsoluting of magma fluids

图8 典型斑岩系统的岩浆房结构特征及其出溶流体迁移路经(据文献[31]略修改)

Fig.8 Structure characteristics of magma chamber in typical porphyry system and migration path of exsolution fluid. Modified from [31].

图9 青藏高原斑岩铜矿成矿流体演化路径(据文献[21]) A为深部岩浆房出溶的超临界流体;B、C分别为超临界流体相分离后形成的低密度富气相和高盐度富液相。虚线表示成矿流体演化路径,阴影表示引起各期蚀变的流体温度、压力范围。

Fig.9 Metallogenic fluid evolution path of porphyry copper deposit in Qinghai-Tibet Plateau. Adapted from [21].

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