The mafic-ultramafic igneous rocks formed due to underplating with crustal stretching during Carboniferous to Permian. The magma underplating during Carboniferous to Permian (330-250 Ma) period heated up the lower crust and thus the crust got hotter. The following cooling crustal episode led to part of the mountain belt sink by thermal subsidence, which ended up forming the Junggar Basin. Another magma underplating event occurred in the Mesozoic era. This was forming heterogenic silica-rich igneous rocks due to the partial melting of numerous oceanic crusts contaminated with mantle wedge. With the influence of Variscan orogeny, Early Permian marine facies changed into the terrestrial environment during Late Permian. This is because orogenic compression and crustal thickening resulted in higher sedimentation and withdrawn of the sea. At that time, widespread uplift occurred with subsidence formed a graben at first. Then, the area gradually became a mountain-trapped peripheral foreland basin due to high-temperature and relaxing subsidence from the regional extension. Some also suggested this landform caused by the combined effect of shearing and extension or thrusting from crustal shortening. Starting from Permian, Junggar Basin was formed to initiate the foreland basin cycle. There presented extensional shearing and continuous deposition of non-marine foreland basin-fill till Triassic. Since the level of the trapped lake in the basin was rising, finer deposits covered widespread the basin with denudation. This also marked as the end of the foreland basin cycle. From Jurassic to Palaeogene, the Junggar Basin undergone intra-continental depression. There was covered in braided delta with few lakes and increasing subsidence rate towards the south from 20 to 120 m/Ma during Jurassic. The collision of the Lhasa block from the south resulted that the delta formed along the margin of the basin. Also, the deeper lake was at the basin centre during Lower Cretaceous. Afterward, the southward lake depression leading the basin centre shift to the south in the Upper Cretaceous period. In Paleogene, braid-delta developed over the basin where sediments entered from the mountains of the surrounding basin. Starting from Neogene, the thrust fault in the Junggar Basin was reactivated. At the same time, there was rapid uplift of Tian Shan since Himalayan orogeny formed by the collision between Indo-plate and Eurasian Plate.