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摘要: 锡作为支撑信息产业、航空航天及国防科技等战略领域的关键矿产，其资源分布在全球极不均匀。开展全球主要锡矿产区对比研究，对理解锡矿成矿规律及全球锡矿勘查和开采具有重要意义。为了更好地理解不同构造背景下锡矿床形成的构造环境及不同类型锡矿床的构造控矿样式，通过系统梳理大陆裂谷和3种汇聚型板块边界典型的锡矿床产出构造环境，并总结了常见锡矿床的构造控矿样式，取得了如下认识：第一，针对热液流体中锡的迁移与锡石沉淀的数值模拟表明，成矿热液未被花岗质围岩完全缓冲是导致锡有效运移和局部富集的关键；这一过程必须依赖高效的构造通道才能实现，从而凸显了构造在热液锡矿成矿中的核心控制作用。第二，无论是在裂谷伸展、安第斯型大陆边缘挤压、西太平洋型大陆边缘弧后伸展以及碰撞造山后伸展哪种构造背景下，热液锡矿床成矿仍符合岩浆热液型锡矿成矿模型的一贯主张，即上述伸展背景下高分异的长英质岩石主导锡成矿作用，伸展/张扭性构造背景有利于热液锡矿床形成。此外，近年部分学者报道了同增生造山过程中变质作用导致锡的预富集，并详细揭示了进变质过程中锡的活化和退变质过程中黑云母绿泥石化释放Sn形成锡石的过程。上述研究为碰撞造山型锡矿成矿理论发展奠定了基础。第三，岩浆热液型锡矿床以矽卡岩型和石英脉型锡矿床为主，通常二者常伴生出现。成锡岩体内部及周缘发育含锡的岩浆冷凝收缩裂隙、水岩分离裂隙、岩浆侵位挤压裂隙和区域构造应力叠加裂隙等。远离成锡岩体受岩石流变学差异或断裂（切层断层和顺层断层）的强烈控制，形成多样的矿化网络结构。根据矿化网络结构内是否发育角砾，可以把含矿脉分为2类。一类是不发育角砾的容矿构造，按复杂程度逐渐增加分为单脉、单脉复合系统、“非”字型脉系统、对称复合脉系统和不对称复合脉系统。单脉的形态及延伸与容矿构造力学性质关系密切。另一类是发育角砾的容矿构造，按复杂程度逐渐增加分为产于剪切带内对称脉、角砾脉系统、脉与顶板网脉复合系统、多角砾脉复合系统。构造序次和构造分异的厘定对热液锡矿床构造控矿作用的研究具有重要作用，加强典型矿床/矿集区构造序次和构造分异的精细填图并结合数值模拟和岩石流变学实验研究是热液锡矿床构造控矿作用研究的发展方向。Abstract:
Objective As a critical mineral supporting strategic sectors such as the information industry, aerospace, and defense technology, tin exhibits an extremely uneven distribution of global resources. Conducting comparative studies on major global tin-producing regions is of great significance for understanding the metallogeny of tin deposits and for global tin exploration. To better comprehend the tectonic settings of tin deposit formation in different structural environments and to understand the structural styles of tin deposits, this paper systematically reviews the tectonic environments of typical tin deposits in continental rifts and three types of convergent plate boundaries (Andean-type continental margin, Western Pacific continental margin, collisional orogenic belt). We summarize the structural styles of tin deposits and present the following findings: Conclusion (1) Numerical simulations of tin transport and cassiterite precipitation from hydrothermal fluids indicate that incomplete buffering of ore-forming hydrothermal fluids by granitic wallrock is a common characteristic of many magmatic-hydrothermal tin deposits. This highlights the importance of structural pathways for hydrothermal tin mineralization. (2) Regardless of the tectonic setting—be it an extensional rift, a compressional Andean-type continental margin, an extensional Western Pacific continental margin back-arc, or an extensional post-collisional tectonic settings—hydrothermal tin mineralization aligns with the magmatic-hydrothermal tin deposit model, which posits that highly fractionated felsic rocks dominate tin mineralization. Extensional/transtensional tectonic settings are favorable for the formation of hydrothermal tin deposits. Additionally, recent studies have reported pre-concentration of tin due to metamorphism during syn-accretionary orogenesis, detailing the release of tin during prograde metamorphism and the formation of cassiterite during retrograde metamorphism through biotite chloritization. These findings lay the groundwork for the development of theories about collision-related tin metallogenesis. (3) Magmatic-hydrothermal tin deposits are primarily skarn-type and quartz vein-type, often occurring together. Within and around tin-bearing intrusion, tin-bearing magmatic cooling contraction fractures, water-rock separation fractures, magmatic emplacement compression fractures, and regional tectonic stress superposition fractures commonly develop. Away from the tin-bearing intrusions, mineralization is strongly controlled by rheological differences in rocks or faults (cross-cutting and bedding-parallel faults), forming diverse structure-mineralization networks. Based on the absence or presence of breccias in the structure-mineralization network, ore-bearing vein structures can be classified into two categories. The first category includes structures without breccias, which, in the order of increasing complexity, are: simple veins, composite simple-vein systems, “lit-par-lit” vein systems, symmetrical complex vein systems, and asymmetrical complex vein systems. The morphologies and extensions of single veins are closely related to the mechanical properties of the host structures. The second category includes structures with breccias, which, in order of increasing complexity, are: anastomosing veins in shear zone systems, brecciated vein systems, vein and hanging-wall stockwork systems, and multiple brecciation vein systems. Significance The determination of tectonic sequences and deformation partitioning plays a crucial role in studying the structural control of hydrothermal tin deposits. Enhancing detailed mapping of structures in typical deposits/districts, combined with numerical simulations and rheological experiments on rocks, represents the future direction for research on structural controls of hydrothermal tin deposits. -
图 1 全球热液锡矿床分布图（据Taylor，1979；杨林等，2023修改）
Figure 1. Map showing the global distribution of tin and tungsten deposits (modified after Taylor, 1979; Yang et al., 2023)
图 2 全球主要锡成矿省产出构造环境示意图（据Taylor，1979修改）
a—陆内裂谷；b—安第斯型大陆边缘；c—西太平洋大陆边缘；d—碰撞造山带
Figure 2. Structural environment of major global tin provinces (modifided after Taylor, 1979)
(a) Intra-continental rifting; (b) Andean-type continental margin; (c) Western Pacific continental margin; (d) Collisional orogenic belt
图 3 南非布什维尔德锡矿集区构造−岩浆−锡矿化特征
a—南非布什维尔德杂岩有关锡矿床构造模型； b—布什维尔德杂岩地质图； c—罗伊贝赫（Rooiberg）锡矿田莱乌波特（Leeupoort）地区矿化−地质剖面（据Vonopartis et al.，2020修改）
Figure 3. Tectonic–magmatic–tin mineralization characteristics of the Bushveld Tin Province, South Africa
(a) Structural Model of the tin deposits associated with the Bushveld Complex, South Africa; (b) Geological map of the Bushveld Complex, South Africa; (c) Section of the Leeupoor region of the Rooiberg tin field (modifided after Vonopartis et al., 2020)
图 4 玻利维亚锡矿带矿化分布图
a—玻利维亚锡矿带主要矿床、岩体及火山沉积分布图；b—玻利维亚锡矿带火山−次火山成因浅成低温热液与异位高温热液矿床示意剖面模型（据Gemmrich et al.，2021修改）
Figure 4. Distribution of the mineralization in the Bolivian Tin Belt
(a) Location of the main ore deposits, plutons, and volcanic deposits along the Bolivian Tin Belt; (b) Schematic cross-section of volcanic- and subvolcanic-hosted epithermal and xenothermal deposits in the Bolivian Tin Belt (modifided after Gemmrich et al., 2021)
图 5 南盘江−右江成矿带地质与锡钨矿床分布图
a—研究区大地构造位置图；b—南盘江−右江成矿带锡金多金属矿集区大地构造位置及锡多金属矿床分布图（Xiao et al., 2022）
Figure 5. Geology and distribution of Sn-W deposits in the Nanpanjiang–Youjiang metallogenic belt
(a) Tectonic map of the study area showing continental blocks and bounding sutures; (b) Schematic geological map of the Nanpanjiang–Youjiang metallogenic belt and the distribution of polymetallic Sn deposits (modified after Xiao et al., 2022)
图 6 喜马拉雅造山带区域构造与错那洞锡钨铍矿床位置图（据吴福元等，2015修改）
Figure 6. Regional tectonic map of the Himalayan Orogenic Belt with the location of the Cainadong tin-tungsten-beryllium deposit (modified after Wu et al., 2015)
图 7 英国康沃尔锡矿集区构造演化与锡矿化样式及矿化分带图
EEC—东欧克拉通；NAC—北美克拉通；CEEP—中欧伸展省a—英格兰西南部康沃尔地区原生锡矿床示意图；b—英格兰西南部康沃尔地区矿化分带示意图（据Taylor，1979修改）；c—基于冈瓦纳大陆与劳伦大陆板块构造背景的欧洲与北非华力西造山运动时序框架（据Kroner and Romer.，2013修改）
Figure 7. Tectonic evolution and tin mineralization patterns and zonation in the Cornwall tin district, southwest England
(a) Diagrammatic representation of primary tin deposit in the south-west of England (Cornwall); (b) Mineralization zonation of Cornwall, south-west of England (modified after Taylor, 1979); (c) Time frame for the Variscan orogeny in Europe and Northern Africa in the plate tectonic context of the interaction of Gondwana and Laurussiad (modified after Kroner and Romer., 2013). Abbreviations: EEC—East European Craton; NAC—North American Craton; CEEP—Central European Extensional Province
图 8 马来西亚半岛古特提斯洋演化过程及岩浆−锡矿床分布图
a—马来西亚半岛简化地质图及锡矿床与花岗岩分布特征；b—马来西亚半岛古特提斯洋演化过程的构造示意模型图（据Yang et al., 2020修改）
Figure 8. Paleo-Tethyan evolution and the distribution of granitoid tin deposits in Peninsular Malaysia
(a) Simplified geologic map of Peninsular Malaysia showing the distribution of tin deposits and granites; (b) Schematic tectonic cartoons showing the Paleo-Tethyan evolution of Peninsular Malaysia (modified after Yang et al., 2020)
图 9 云英岩型和斑岩型锡矿床示意图
a—玻利维亚锡矿带斑岩型矿床构造蚀变系统（据Sillitoe et al.，1975修改）；b—云英岩模型（据Pirajno，1992修改）
Figure 9. Schematic diagram of porphyry and greisen tin deposits
(a) Composite reconstruction of a typical Bolivian tin deposit system (modified after Sillitoe et al., 1975); (b) A model of greisen formation (modified after Pirajno., 1992)
图 10 矽卡岩型锡矿床构造控矿样式
a—美国加利福尼亚州内华达山脉深成岩接触带与矽卡岩体的关系；b—碳酸盐岩夹层层间交代矽卡岩构造控矿样式；c—碳酸盐岩顺层交代矽卡岩构造控矿样式；d—碳酸盐岩与砂岩Si-Ca界面矽卡岩构造控矿样式；e—花岗岩接触带矽卡岩构造控矿样式（据Kwak，1987修改）
Figure 10. Ore-bearing structural styles of skarn tin deposits
(a) Relationship between plutonic contacts and skarn bodies in the Sierra Nevada Mountains, California, USA; (b) Structural style of interbedded skarn in carbonate rocks; (c) Structural style of skarn in stratiform carbonate rocks; (d) Structural style of skarn at the Si–Ca interface; (e) Structural style of skarn at the contact between granite and carbonates (modified after Kwak, 1987)
图 11 石英脉型锡矿床构造控矿样式
a—广西平那钨锡矿床锡石−白云母−石英脉；b—广西平那钨锡矿床石英−黑钨矿脉与锡石−白云母−石英脉产于同−含矿构造空间；c—广西大厂矿田黑钨矿−石英脉与辉锑矿−铁白云石脉产于同一容矿裂隙
Figure 11. Ore-bearing structural styles of quartz vein type tin deposits
(a) Cassiterite–muscovite–bordered quartz vein from the Pingna W–Sn deposit, Guangxi; (b) Quartz–wolframite vein and cassiterite–muscovite–bordered quartz veins coexist within the same ore-bearing fracture from the Pingna W–Sn deposit; (c) Wolframite–quartz and stibnite–ankerite veins occur within the same ore-bearing fracture from the Dachang district, Guangxi
图 12 含锡矿脉矿化网络结构（据Hosking, 1988修改）
Figure 12. Tin-bearing vein structures (modified after Hosking, 1988)
图 13 广西百色平那钨−锡矿床不同地质体磁化率与石英脉型钨−锡矿脉关系
N—样本数量a—广西百色平那钨−锡矿床不同地质体磁化率统计图；b—石英脉型钨−锡矿化顶底板围岩磁化率分布特征
Figure 13. The relationship between the magnetic susceptibility of geological units and quartz-vein type tungsten–tin veins in the Pingna W–Sn deposit, Baise, Guangxi
(a) Magnetic susceptibility of different geological bodies in the Pingna tungsten–tin deposit, Baise, Guangxi; (b) Magnetic susceptibility of host rocks in the footwall and hanging wall of quartz vein-type tungsten–tin mineralization
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