Many ophiolites are developedin the western part of the Paleo- Asian Ocean tectonic domain, situated between the Eastern European craton, the Siberian craton and the Tarim craton. According to the spatial and temporal distribution characteristics, these ophiolites can be divided into the following ten zones: ① Yenisei ophiolitie bel, ② Kuznets- West Sayan- Lake ophiolite belt, ③ Salayer- Altai ophiolite belt, ④ Zaysan- South Mongolia ophiolite belt, ⑤ East Kazakh- West Junggar ophiolite belt, ⑥ East Junggar ophiolite belt, ⑦ Northern Tianshan ophiolite belt, ⑧ Naman- Jalayal ophiolite belt, ⑨ Terskyi ophiolite belt, ⑩ Ural- Southern Tianshan ophiolite belt, etc. The ophiolite assemblages in these zones are mostly incomplete, accompanied by pyroclastic rocks, and the mantle rocks are dominated by harzburgite+dunite+lherzolite. The chronology of the ophiolite indicates that the evolution of the ancient ocean basin occurred within a limited time frame of approximately 80~60 Ma, reflecting the restricted scale of the ocean basin. The ancient ocean basin marked by the Kuznets- West Sayan- Lake ophiolite belt is the first generation of the Paleo- Asian Ocean, which began in the Ediacaran period. The second generation of Paleo- Asian Ocean is marked by the most widely distributed Cambrian- Ordovician ophiolites, showing a tectonic pattern of micro- blocks alternate with small ocean basins. The third generation Paleo- Asian Ocean mainly refers to the Devonian- Early Carboniferous Zaysan Ocean and the Ural- Southern Tianshan Ocean. There is no paleo- ocean that evolved continuously from the Early Paleozoic to the Late Paleozoic. The subduction orogeny of the Paleo- Asian Ocean was mainly achieved through the closure of several small ocean basins. The collision did not involve a direct interaction between the Siberia and Gondwana continents; rather, it occurred through the interaction of micro- blocks. Therefore, the orogeny was not strong, leading to a scarcity of large- scale nappe structures beyond the tectonic belt.