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

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

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.

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.

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].

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

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.

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].

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].

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

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

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.

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

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.

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