South China Block is situated in the Eastern Asian margin. Its tectonic process was constrained by convergences of the ancient South China, paleo-Asian, paleo-Tethys and paleo-Pacific oceans with different ages. Studies suggest that this block was initially formed by the Neoproterozoic subduction-accretion of ancient South China Ocean and the assembly of the Yangtze and Cathaysia blocks. Then, this block experienced three crucial tectonic-magmatic events happened in Phanozoic. Among these events, the Neoproterozoic and Late Mesozoic tectono-magmatism were trigged by convergences of the ancient South China and paleo-Pacific oceans, while the Silurian and Triassic events took place under intracontinental settings that were strongly affected by convergences of the paleo-Asian and paleo-Tethys oceans, respectively. The South China Block had a complicated evolutionary history of subduction-accretion and collision in 980-820 Ma, forming the Jiangnan Orogenic Belt and the proto-South China Continent followed by a rifting tectonics and bimodal volcanism in 810-760 Ma. From 760 to 460 Ma, the entire South China Block was situated under a shore, shallow sea to slope depositional environment. During 460-400 Ma, as a response of paleo-Asian Ocean convergence, an intracontinental orogeny had generated the South China Orogenic Belt. Shortly afterwards, this block underwent a stable carbonate deposition in 400-230 Ma under a shore and shallow sea environment. In 240-220 Ma, as responses of paleo-Tethys convergence, intracontinental deformation and S-type granitic magmatism took place. During the early Cretaceous, a basin-and-range framework occurred in the western shore of paleo-Pacific Plate. This paper also discusses several long-lasting hotly debated topics.

A systematic dataset of petrography, mineralogy, geochronology, and geochemistry is reported for the enclave-bearing calc-alkaline I-type granitoids from the Chinese Altai, Central Asian Orogenic Belt (CAOB). Zircon U–Pb dating and geochemical data indicate that the MME and granitoids formed coevally at ~395 Ma in a subduction setting. Geochemical modelling and hybrid testing suggest that the granitoid parental magma was formed by mixing between a mafic and a felsic endmember that can be identified by isotopic compositions. The mafic rocks have (87Sr/86Sr)i of 0.7048 – 0.7062, εNd(t) of -0.5 – +2.6, and zircon εHf(t) of +2.3 – +5.4, while the host granitoids have similar Sr isotopic compositions ((87Sr/86Sr)i = 0.7054 – 0.7064), but generally lower whole-rock εNd(t) and zircon εHf(t) values (-2.2 – +0.4 and +0.6 – +4.6, respectively). The sharp decrease of An values from cores to rims (e.g., from ca. 80 to 40) of plagioclase phenocrysts points to polybaric crystallization accompanied by degassing, which is supported by the pressure and water content estimations based on amphibole compositions. Petrographic evidence and plagioclase in-situ Sr isotopic compositions ((87Sr/86Sr)i = 0.7053 - 0.7071) confirm the interaction of two isotopically different magmas during the mineral crystallization. A model for the formation of the enclave-bearing calc-alkaline plutons in an arc setting is presented: in-depth mantle and crustal melting and efficient magma mixing controlled the principal chemical compositions of the granitoid intrusions, while the later decompression-dominated crystallization, magma mingling and limited mixing in the higher crustal level finally determined the texture, mineral composition, and enclave morphology.