Anatectic Metamorphism and Granite Petrogenesis in Continental Collision Zones
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摘要: 大陆碰撞带是地壳岩石发生深熔变质和花岗岩浆作用的重要场所，也是超大陆发生聚合和裂解过程的关键位置.对深熔变质作用的理解有助于揭示地壳分异过程和花岗岩成因等诸多问题，同时对威尔逊旋回过程中超大陆动力学的理解有重要启示.在大陆碰撞过程的不同阶段，其动力体制会从挤压变成拉张，地温梯度会由低变高，从而形成时空分布不同、矿物组合各异的变质岩和岩浆岩.在大陆碰撞和俯冲的挤压阶段，变质温压比值较低，只有硬碰撞引起的地壳加厚产生的高压麻粒岩相变质作用以及深俯冲导致的超高压变质作用，不会发生深熔变质作用.在大陆深俯冲结束之际，板块界面动力体制由挤压变为拉张，受到超高压变质的地壳会以岩片状沿俯冲隧道发生逆冲折返.在大陆碰撞后阶段，一旦碰撞带岩石圈地幔发生减薄，软流圈地幔上涌导致主动张裂，上覆地壳就会在高的地温梯度下发生巴肯型深熔变质作用，从而形成大量的花岗岩.因此，地壳深熔变质和花岗质岩浆的发育程度与岩石圈厚度的变化密切相关.虽然幔源镁铁质岩浆结晶分异作用是大洋俯冲带之上花岗岩形成的常见方式，但是地壳部分熔融才是大陆碰撞带花岗岩浆作用的典型方式.地壳岩石性质是形成不同类型花岗岩的关键，Ⅰ型和S型花岗岩分别主要来自于变火成岩和变沉积岩的部分熔融，而A型花岗岩则起源于堆晶或残留体的部分熔融.脱水熔融和水化熔融是产生花岗岩浆的两种基本物理化学机制，二者可在同一区域内发生，构成脱水‒水化耦合的部分熔融机制.大陆碰撞带作为古板块缝合带，也是构造薄弱带，易于发育大陆主动张裂，这是在碰撞后阶段深部陆壳脱水‒水化耦合熔融直至浅部陆壳部分熔融的主要构造机制，结果形成花岗岩‒混合岩‒麻粒岩高温岩石组合.一般来说，超大陆聚合阶段与碰撞挤压背景下的变质作用相关，而超大陆裂解与主动张裂拉张体制下的变质作用相关.虽然大陆张裂未必都能成功，但是其中夭折张裂在业已汇聚板块边缘最为常见.因此，夭折大陆张裂与陆内深熔变质作用和花岗岩浆作用之间的关系最为密切，这也是正确认识超大陆聚合之后到裂解之前陆内地质过程与构造演化之间关系的关键.Abstract: Anatectic metamorphism develops from high-grade metamorphism to crustal anataxis, marking population of extensional tectonism in continental collision zones. It is much more related to breakup than assembly of supercontinents in both space and time.Deciphering the anatectic metamorphism is critical to understand the tectonic evolution of continental collision zones in the late stage. It is substantial to resolve not only petrological problems such as crustal differentiation and granite petrogenesis but also tectonic problems such as supercontinent geodynamics in Wilson cycles. In general, continental collision zones may change their dynamic regime from compression to extension and their geothermal gradient from low to high during their evolution from the early to late stages. This results in different types of metamorphism and magmatism with given occurrences in both time and space. Alpine type metamorphism is caused by compressional heating at low geothermal gradients during subduction of one lithosphere beneath the others, and Barrovian type metamorphism occurs at moderate geothermal gradients due either to compressional heating during collisional thickening of the crust or to extensional decompression during nearly isothermal exhumation of the deeply subducted crust. In contrast, Buchan type metamorphism is caused by extensional heating at high geothermal gradients during continental rifting. Because of the anatectic metamorphism, granites are produced together with migmatites and granulites in the post-collisional stage. Therefore, granitic magmatism is the endmember product of anatectic metamorphism consequential to thinning of the thickened lithospheric mantle. Both processes are closely associated with the change of lithospheric thickness along continental collision zones. Although granites above oceanic subduction zone are mainly produced by fractional crystallization of mantle-derived mafic magmas, partial melting of crustal rocks is the dominant way to generate granitic magmas in continental collision zones. In particular, the source nature of crustal rocks is a key to the composition of granites. Ⅰ-type and S-type granites are primarily derived from partial melting of metaigneous and metasedimentary rocks, respectively. In comparison, A-type granites are derived from partial melting of either cumulates or restites. Dehydration and hydration melting are two fundamental mechanisms to produce granitic magmas. They can occur simultaneously at the same zones, leading to dehydration melting in the deeper crust and hydration melting in the shallower crust. Upwelling of the asthenospheric mantle consequential to thinning of the lithospheric mantle is a common geodynamic mechanism for continental active rifting, giving rise to the dehydration-hydration coupled melting to produce granite-migmatite-granulite associations in continental collision zones. As a consequence, supercontinent assembly is associated with compressional metamorphism during continental collision, whereas supercontinent breakup is associated with extensional metamorphism during active rifting. Continent rifting may not succeed but fail, resulting in anatectic metamorphism and granitic magmatism at convergent plate margins. Therefore, the failed continental rifting is a key process in linking the types of regional metamorphism to the tectonic evolution of continental collision zones from supercontinent assembly to breakup.
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图 1 大陆碰撞带软碰撞(浅俯冲)形成增生楔示意图(修改自Zheng et al., 2005)
Fig. 1. Schematic diagram showing the formation of accretionary wedge during continental soft collision (shallow subduction)
图 2 汇聚大陆边缘两类挤压构造示意图(修改自郑永飞等, 2022)
大陆板块俯冲之前首先是大洋板块俯冲，然后或者是大陆地壳硬碰撞加厚（图a）、或者是大陆地壳深俯冲到岩石圈地幔深度（图b）
Fig. 2. Schematic diagrams showing the two types of compressional tectonics at converging continental margins
图 3 喜马拉雅造山带岩相构造单元分布示意图(修改自Zhang et al., 2012)
岩石构造单元缩写：SG.Siwalik沉积建造；LHS.小喜马拉雅低级变质岩；GHS.大喜马拉雅高级变质岩‒淡色花岗岩；THS.特提斯喜马拉雅增生楔；YZS.雅鲁藏布缝合带；GD.片麻岩穹窿.断层缩写：STD.藏南拆离断层；MCT.主中逆冲断层；MFT.主前锋逆冲断层；MBT.主边界逆冲断层；GCT.大中逆冲断层
Fig. 3. Schematic diagram showing the occurrence of lithotectonic units in the Himalayan orogen
图 4 大别造山带岩相构造单元分布示意图(修改自Zheng et al., 2019)
Fig. 4. Schematic diagram showing the occurrence of lithotectonic units in the Dabie orogen
图 5 汇聚板块边缘变质相系与地温梯度关系图解(修改自Zheng and Chen, 2021)
图中矿物反应或矿物相变才是标志变质相系的边界：阿尔卑斯型与巴罗型变质相系之间以钠长石分解形成硬玉和石英为界（Zheng and Chen，2017），巴罗型与巴肯型变质相系之间以铝硅酸盐同质多像转变为界（Zheng and Chen，2021；Pattison and Goldsmith，2022）.矿物缩写：Ab. 钠长石；And. 红柱石；Coe. 柯石英；Jd. 硬玉；Ky. 蓝晶石；Sil. 夕线石；Qz. 石英
Fig. 5. The thermodynamic relationship between metamorphic facies series and geothermal gradients at convergent plate margins
图 6 大陆碰撞带地壳变质P-T轨迹示意图(底图修改自Zheng and Chen, 2021)
图中矿物缩写：Ab. 钠长石；And. 红柱石；Coe. 柯石英；Jd. 硬玉；Ky. 蓝晶石；Sil. 夕线石；Qz. 石英
Fig. 6. Schematic diagram showing the metamorphic P-T paths of crustal rocks in continental collision zones
图 7 大陆碰撞带超高压地体三类变质P-T轨迹(修改自Faryad and Cuthbert, 2020)
a.降温降压，对应于超高压岩片沿俯冲隧道快速折返；b.等温降压，对应于超高压岩片沿俯冲隧道缓慢折返；c.降压加热，对应于超高压地体以穹窿式抬升.矿物名称缩写：Coe.柯石英，Dia.金刚石，Gra.石墨，Qz.石英.图中字母缩写表示不同名称的大陆碰撞带：DS.中国中东部的大别‒苏鲁造山带，KM.哈萨克斯坦的Kokchetav地体，SM1.土耳其中部的Sivrihisar地体，WD、WS.西阿尔卑斯的Dora Maira地体和Sesia带；AT.中国西北的阿尔金带，D1.中国中东部的中大别带，EG.波希米亚地体的Erzgebirge，NQ.中国西部的柴北缘，PL.西阿尔卑斯的Piemonte Ligurian，WM.西阿尔卑斯的Monviso带；D2.中国中东部的北大别带，LD.中阿尔卑斯的Lepontin穹窿，ME.波希米亚地体的Moldanubian榴辉岩带，MG.波希米亚地体的Moldanubian麻粒岩带，NG.新几内亚，SM2.土耳其中部的Sivrihisar地体，WG.挪威西片麻岩省
Fig. 7. Three types of metamorphic P-T paths for ultrahigh-pressure terranes in continental collision zones
图 8 汇聚板块边缘双变质带形成机制和P-T轨迹卡通图(修改自Zheng and Chen, 2021)
a.板片汇聚期间大洋或大陆岩石圈的冷俯冲产生较低T/P变质带和顺时针P-T轨迹；b.板片汇聚之后减薄造山带岩石圈的热张裂作用产生较高T/P变质带和顺时针或逆时针P-T轨迹
Fig. 8. Schematic cartoons for the formation mechanism and P-T path of paired metamorphic belts at convergent plate margins
图 9 大陆碰撞带两阶段构造演化模式图(引自Zheng and Gao, 2021)
a.早期阶段：大陆俯冲导致挤压体制和地壳加厚，此时俯冲板片与地幔楔保持耦合，地壳变质作用发生在低热梯度下；b.晚期阶段：俯冲板片回卷导致俯冲板片与地幔楔之间解耦，深俯冲地壳折返甚至减压熔融，此时处于高热梯度和伸展条件
Fig. 9. Schematic diagrams for the two-stage tectonic evolution of continental collision zones
图 10 岩石圈厚度对变质脱水和地壳深熔的影响(引自Zheng and Gao, 2021)
a.碰撞造山作用导致造山带岩石圈被加厚；b.造山带岩石圈地幔减薄，软流圈地幔上涌，导致主动型张裂作用，加厚地壳发生大规模部分熔融，形成花岗岩‒混合岩‒麻粒岩组合；c.加厚地壳经剥蚀作用而减薄，恢复至正常厚度，大陆岩石圈进入成熟阶段
Fig. 10. The effect of lithospheric thickness on metamorphic dehydration and crustal anatexis
图 11 大陆碰撞带岩石圈加厚与减薄导致大陆主动张裂(修改自Zheng and Chen, 2021)
a.大陆岩石圈碰撞挤压加厚引起地壳发生巴罗型变质作用；b.加厚岩石圈地幔减薄伸展引起地壳发生巴肯型变质作用
Fig. 11. Schematic diagrams showing the thickening and thinning of the lithosphere and their effect on continental active rifting along continental collision zones
图 12 花岗岩成因上的两种物理化学机制示意图(修改自Moyen et al., 2021)
a.幔源镁铁质岩浆结晶分异形成长英质岩浆；b.地壳部分熔融产生长英质岩浆
Fig. 12. Schematic diagrams showing two types of physical mechanisms for the origin of granites
图 13 汇聚板块边缘花岗岩I-S-A分类与源区性质关系示意图
Fig. 13. The relationship in granite petrogenesis between I-S-A classification and source nature
图 14 澳大利亚拉克兰造山带古生代花岗岩Sr-Nd同位素组成关系(修改自Zheng and Gao, 2021)
Fig. 14. The Sr-Nd isotope compositions of Paleozoic granites from the Lachlan orogen in Australia
图 15 汇聚板块边缘花岗岩成因中的两组分混合关系示意图
缩写AFC代表同化分异结晶；MASH代表同化‒混合‒储存‒均一化
Fig. 15. Two-component mixing in petrogenesis of granites at convergent plate margins
图 16 地壳深熔作用产生的花岗岩中不同种类锆石的成因(引自Zheng and Gao, 2021)
图中内部和外部轨迹分别代表固相线之下和固相线之上的锆石行为
Fig. 16. Origin of different types of zircon in granites produced by crustal anatexis
图 17 地壳在主动型张裂作用条件下因软流圈地幔上涌加热导致的脱水和水化熔融模式图（引自Zheng and Gao，2021）
图中脱水熔融发生的外部热量来源于因大陆碰撞带岩石圈去根作用所引起的软流圈地幔上涌，而水化熔融是由下伏地壳受热脱水产生的外来流体所诱发
Fig. 17. Schematic diagram showing the coupled dehydration and hydration melting of the crust during active rifting consequential to asthenospheric heating
图 18 威尔逊旋回构造演化示意图(修改自Zheng and Chen, 2021)
Fig. 18. Schematic diagrams showing the tectonic evolution in a Wilson cycle
图 19 超大陆裂解的两类地球动力学构造机制示意图(修改自Zheng and Chen, 2021)
Fig. 19. Schematic diagrams showing the two types of geodynamic mechanism for supercontinent breakup
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