大陆碰撞成矿作用:新认识与新进展

doi:10.13745/j.esf.sf.2025.4.49

摘要/Abstract

摘要：

大陆碰撞成矿理论框架已经初步构建,但在碰撞带岩石圈结构与深部致矿过程、碰撞带热状态与成矿差异控制、关键成矿过程与矿床成因机理等方面仍认识不足。近年来,通过地球物理-地球化学-岩石学-成矿学等多学科交叉研究和实验模拟,大陆碰撞成矿作用研究取得了诸多新认识和新进展。研究表明,碰撞带可以分为冷碰撞和热碰撞两种基本类型。其中,比利牛斯、阿尔卑斯和加里东造山带为冷碰撞演化序列代表,扎格罗斯、喜马拉雅和华力西造山带为热碰撞演化序列代表。冷/热结构受控于碰撞带深部过程和地幔热扰动强度。碰撞前大洋俯冲对上覆岩石圈的改造,导致岩石圈地幔交代富集、新生下地壳形成和古老地壳活化再造,为碰撞期含铜、金、稀土等岩浆系统形成提供了重要物源。碰撞期软流圈上涌交代、改造、吞噬上覆岩石圈,导致强烈的壳幔物质能量交换,为碰撞成矿提供了深部动力机制。碰撞成矿作用主要形成斑岩铜金矿床、MVT铅锌矿床、碳酸岩型稀土矿床、造山型金矿床以及淡色花岗岩有关的稀有金属矿床等。碰撞型大型斑岩铜矿床的形成要求:大陆板片中缓角度俯冲、俯冲板片垂向撕裂、新生下地壳部分熔融和壳内硫化物分解;MVT超大型铅锌矿的形成要求:褶冲系和前陆带环境、压/张构造转换、盆地卤水沿拆离带的迁移汇聚和前锋带的构造圈闭;碳酸岩型稀土矿床的形成要求:富稀土沉积物俯冲循环、碳酸岩化地幔根部分熔融、富REE碳酸岩浆壳内演化、高密度盐熔体与围岩交代反应;造山型金矿床的形成要求:岩石圈立交桥结构与壳/幔解耦变形、富水幔源超钾质岩浆集聚与去气、流体沿超壳断裂迁移与交代;与淡色花岗岩有关的稀有金属矿床的形成要求:活化改造地壳的部分熔融、拆离构造驱动的岩浆分异或者热驱动的岩浆高度分异。基于上述要素,结合典型矿床对比,建立和完善了大陆碰撞带4种典型矿床的成矿模型。

关键词: 大陆碰撞, 新生下地壳, 俯冲角度, 板片撕裂, 岩石圈架构, 成矿作用

Abstract:

The theoretical framework for metallogenesis in collisional orogen belts is established, yet aspects like lithospheric architecture, deep mineralization processes, thermal regimes and ore genesis mechanisms require refinement. Interdisciplinary research and experimental simulations have greatly improved our understanding of collision-related metallogenesis in orogenic systems. Our research demonstrates that collision zones can be divided into two fundamental types: cold- and hot-collisions. The former includes the Pyrenean, Alpine, and Caledonian orogenic belts, while the latter includes the Zagros, Himalayan, and Variscan orogenic belts. The distinction between these regimes is primarily controlled by lithospheric thermal states and geodynamics. Pre-collision oceanic subduction modifies overlying lithosphere via mantle refertilization, juvenile lower crust formation, and crustal reworking, controlling Cu-Au-REE magmatism during subsequent collision. Asthenospheric upwelling drives crust-mantle exchange, providing deep metallogenic drivers. Mineral deposits within collisional orogen belts include porphyry Cu-Au deposits, Mississippi Valley-type (MVT) Pb-Zn deposits, carbonatite-associated REE deposits, orogenic Au deposits, and rare metal deposits related to leucogranites. The key factors for the formation of collisional giant porphyry Cu deposits include: moderately dipping continental subduction, vertical slab tearing, juvenile lower crust anatexis, and sulfides remobilization. The major factors for the formation of MVT Pb-Zn deposits include: fold-thrust belt, transpression or extension environments, basinal brine migration along detachments, and structural traps. The formation of carbonatite-associated REE deposits is related to the recycling of REE-enriched sediments via subduction, partial melting of carbonate-rich mantle sources, crustal magma evolution, and wall-rock metasomatism by saline melts. The main factors for the formation of orogenic Au deposits include: trans-lithospheric architecture and crust-mantle decoupling, accumulation and devolatilization of volatile-rich, mantle-derived ultrapotassic magma, and fluid flux along crustal-scale faults. Leucogranite-related rare metal deposits form through anatexis of fertile crust and magma differentiation facilitated via heat advenction along detachments. Metallogenic models for these deposit types are refined through comparative analysis.

Key words: continental collision, juvenile lower crust, subduction angle, slab tearing, lithospheric architecture, metallogenesis

中图分类号:

P611

侯增谦, 杨志明, 张洪瑞, 王瑞, 宋玉财, 刘琰, 郑远川, 许博, 王庆飞, 刘英超. 大陆碰撞成矿作用:新认识与新进展[J]. 地学前缘, 2025, 32(6): 179-209.

HOU Zengqian, YANG Zhiming, ZHANG Hongrui, WANG Rui, SONG Yucai, LIU Yan, ZHENG Yuanchuan, XU Bo, WANG Qingfei, LIU Yingchao. Metallogenesis in collisional orogens: New insights and advances[J]. Earth Science Frontiers, 2025, 32(6): 179-209.

图/表 15

图1 比利牛斯-阿尔卑斯-扎格罗斯-喜马拉雅碰撞造山链主要碰撞矿床分布

Fig.1 Distribution of collision-related mineral deposits within the Pyrenees-Alps-Zagros-Himalaya mountain chain

图2 冷/热碰撞带造山结构与矿化类型

Fig.2 Schematic illustration of cold- and hot-collision orogens and associted mineral deposits

图3 冷、热碰撞带热结构与演化序列 a—显示阿尔卑斯和青藏高原变质岩和火山岩包体的温度-压力资料[54];b—反映不同碰撞造山带的温度与山体规模的关系。

Fig.3 The thermal regime and evolution sequence of cold and hot collisional orogen. (a)—p-T conditions of metamorphic rocks and xenolith data from the Alpine and Himalayan-Tibetan collisional orogens[54]; (b)—the relationship between orogenic tempearature and magnitude for the typical collisional orogens.

图4 青藏高原东南缘岩石圈地震速度结果(a)与岩石圈地幔的Mg#变化(b) a—显示120 km深度vP结构、印度大陆岩石圈俯冲前缘位置(ICS-F,灰线)、地震各相异性(SKS)反映的上地幔物质运动方向(黑线)、岩石圈/软流圈界面(LAB)等值线(白线)。红色的粗虚线反映了俯冲的印度板片撕裂带位置。b—显示根据地震速度、大地热流值和地幔岩(包体)橄榄石成分反演的现今岩石圈地幔的Mg#值变化。

Fig.4 The P-velocity image (a) and Mg# ratios (b) of the lithospheric mantle beneath the southeastern Tibetan Plateau. (a) A slice of P-velocity image at depth of 120 km showing Indian continental subducted frontier (ICS-F, dark lines), mantle flow (black lines) measured by SKS splitting analysis, the lithosphere-asthenosphere boundary (LAB, white lines), and tear position of the subducted Indian slab. (b) Mapping of lithosphere mantle Mg# values calculated from seismic velocity, terrestrial heat flow and olivine xenoliths.

图5 不同碰撞造山带Hf同位素填图结果及其所反映的岩石圈物质架构 (据文献[77]) A—伊朗高原;B—青藏高原;C—秦岭造山带。

Fig.5 Zricon Hf isotope contour map showing the lithospheric architecture of the collisional orogens in Iran (A), Tibet (B) and Central China (C). Adapted from [77].

图6 穿越西藏东部岩石圈的两条P波地震剖面成像与重建的岩石圈热结构

Fig.6 Two vertical profiles show the P-wave velocity images and thermal states of the lithosphere in east Tibet

图7 大陆板片中缓角度俯冲、新生下地壳熔融与斑岩铜矿形成

Fig.7 Relationship among subduction angle of continental slab, melting of the juvenile lower crust and generation of porphyry Cu deposits a—A cartoon showing the low- and moderate-angle subduction of the Indian continent-slab during the Cenozoic collision, which resulted in a thermal regime with heat-crust and cold mantle; b—The collisional process triggered partial melting of the juvenile mafic lower crust, and generated potassic adakitic magmas with assicated collision-related porphyry Cu deposits.

图8 特提斯构造-成矿域大陆碰撞造山带MVT铅锌矿区构造演化、铅锌成矿、油气成藏的时间关系(据文献[52-53])

Fig.8 The temporal relationship among evolution of regional deformation, timing of MVT mineralization and hydrocarbon reservoir in the collisional zone witnin the Tethyan metallogenic domain. Adapted from [52-53].

图9 大陆碰撞带褶皱-逆冲带MVT成矿流体迁移机制(据文献[145])

Fig.9 A cratoon showing the migration and discharing of ore-forming fluids along the intra-crustal detachment zone beneath the collision-induced fold and thrust system for the formation of MVT deposits. Adapted from [145].

图10 特提斯大陆碰撞造山带MVT铅锌矿床储矿样式及代表性矿床(据文献[16,153-156])

Fig.10 Characteristic ore traps and their controls on typical MVT deposits within fold and thrust belts. Adapted from [16,153-156].

图11 大陆碰撞褶皱-逆冲系MVT铅锌矿床3阶段演化成矿模型(据文献[156])

Fig.11 Three-stage model for Mississippi Valley-type Zn-Pb mineralization in the collision induced fold- thrust system. Adapted from [156].

图12 俯冲带REE迁移方式与大陆岩石圈地幔交代富集机制显示出来自俯冲带的富REE熔/流体(a)和富REE底辟体(b)对成矿物质的输运方式 SCLM:大陆岩石圈地幔。

Fig.12 Schematic illustration showing the transfer of REE and metasomatised enriched lithospheric mantle in subduction zone. The REE may be migrated as CO2-rich fluids and melts (a) or diapirs (b) to overlying mantle wedge. SCLM: subcontinental lithospheric mantle.

图13 碰撞带碳酸岩型REE矿床成矿过程(据文献[182])

Fig.13 Schematic illustration showing the ore-forming processes of the carbonatite-associated rare earth deposit in collision zone. Adapted from [182].

图14 哀牢山金矿带岩石圈立交桥结构与造山型金成矿作用(据文献[206]) (a)—地表GPS和岩石圈地幔的SKS探测表明北西向地壳运动(地表白色箭头)与东西向地幔运动(地幔黑色线段)形成立交桥结构,板片回撤引发软流圈上涌并诱发富集地幔熔融,富水基性岩浆在壳幔解耦界面处停留-聚聚-成池-去气;(b)—底侵的基性岩浆发生脱气与硫化物熔离,形成含金流体沿区域剪切带向上输运并沉淀成矿。

Fig.14 Schematic illustration showing the overpass-type lithosphere architecture and its control on the orogenic gold depositsin the Ailaoshan gold belt. Adapted from [206]. (a) The overpass type lithosphere architecture is constituted by surface NW-trending deformation (white arrows) as shown by GPS and E-W-trending flow of mantle lithosphere (black lines) as shown by SKS splitting analysis. Slab rollback induced upwelling of hot asthenosphere and partially melting of the enriched mantle. The produced basic magma ponded and degassed at the boundary of crust-mantle decoupling. (b) The Au-bearing fluid was derived from degassing and sulfide separation of the underplated basic melts, and migrated along regional shear zone and finally precipated to form gold deposit.

图15 腾冲地块俯冲型与碰撞型锡矿床的成矿构造模型图(据文献[235])

Fig.15 Tectonic model for the formation of subduction-related and collision-related Sn deposits in the Tengchong block. Adapted from [235].

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