A large number of previous isotopic geochronology and isotopic tracing studies show that there are four landmasses with different ages in northern Xinjiang, namely Tarim landmass-with Archean basement; Tianshan massif-based on Proterozoic; Junggar block has a Mesoproterozoic-Neoproterozoic basement; Altai block-has a basement of Proterozoic-Mesoproterozoic. The geological history of northern Xinjiang should be traced back to 3300~3000Ma at the earliest. A set of Proterozoic complex in Kuruktag area on the northern margin of Tarim block constitutes the Proterozoic primitive continental core in western China, which can echo other continental cores in Eurasia. The paleo-Mesoproterozoic continental core of Tarim block gradually expanded and matured through structure, metamorphism and magmatism about 2800Ma and 2500Ma ago, forming the ancient basement of Tarim block. The Sm-Nd isochron age of mixed migmatized amphibolite in Gambulak mining area is 2453Ma, and εNd(t)=+2. The Pb isotopic age of a single zircon in the blue granite unconformity covered by Sinian in Xishankou area is (2487.7 5.1) Ma (high, 1990), and the continental crust is further enlarged (for example, the Rb-Sr isochron age of the whole gneiss in southern Tsinger is 2028Ma±82Ma). After the Tsinger Movement (about 2500~2400Ma ago), it entered the stage of Proterozoic evolution. With the gradual expansion of the ocean, huge terrigenous clastic rocks and carbonate rocks have been deposited, and volcanic eruptions have occurred in some areas. Xingditage Group is the first Proterozoic caprock unconformity covered on Archean complex, and its bottom age is determined by Pb-Pb isochron age as (2399±33)Ma, ε nd (t) =+4.3. About 2000 ~ 1900 Ma ago, during the land reclamation period, regional metamorphism generally occurred in the northern margin of Tarim, and a large number of migmatized granites were formed, which made an important crust-mantle differentiation event form the nearly east-west Tianshan basement about 2000 ~ 1800 Ma ago. The Sm-Nd isochron age obtained from the metamorphic rock series of Xingxingxia Group in the eastern Tianshan Mountains is 1727Ma, and ε nd (t) =+5.3. The Sm-Nd model age of some granites indicates the existence of this crustal proliferation event, which is consistent with a crustal tectonic movement widely occurring in the world.

The basement of Altai massif was also formed in this period. Sm-Nd isotopic ages of a series of granites, volcanic rocks and metamorphic rocks in Altai area are mostly in the range of 1600 ~ 1400Ma, which is consistent with the ages of metamorphic rocks exposed near Fuyun and zircon U-Pb ages extending westward to Kazakhstan. Therefore, it may reflect the crustal residence time of basement materials. Considering the "mixing" factor, 1600 ~ 1300 Ma should be the lowest age of basement paleocrustal material, that is, the basement of Altai should be at least Mesoproterozoic. How (1989) obtained the U-Pb age of 1800 ~ 2400 Ma from the Dengli granite gneiss in Dahan, Fuhai County. In this paper, the genesis of Attish granite body in northern Altai is discussed by using lead isotopes, and the crust-mantle differentiation time of 207 1Ma is calculated, which reflects the formation time of crust in Altai area. Therefore, the Altai block should have a Proterozoic basement.

About 1600Ma ago, after entering Mesoproterozoic, Tianshan and Tarim regions had different characteristics. Erjigan Group in the northern margin of Tarim block is unconformity covered on Xingditage Group. The Pb-Pb isochron ages of Aksu Group, which is exposed gently in Kepingtage, are (166316) Ma and (1596 66) Ma, respectively, which can be used as a record of this geological historical time. The Tianshan area lacks isotopic age records of geological processes in this period. But by the middle of Mesoproterozoic, that is, the end of the Great Wall, large-scale structure, magma and metamorphism had taken place in the area north of Tianshan Mountain. In the western Tianshan Mountains, the Tekes Group, which was in a relatively stable sedimentary environment during the Great Wall period, produced folding movement, which was covered by the unconformity of Su Qun in Jixian County. In the Tianshan active area, a large number of age data of about 1400Ma have been obtained, such as Rb-Sr isochron age of Aikendaban siliceous rocks in Hejing County (Zhu et al., 1986). In addition, metamorphic rocks such as migmatized gneiss distributed along the east-west direction near Fuyun in Altai area may also be continental crust produced by crust-mantle differentiation in this period, but there is no geological evidence to support the geological process of about 1400Ma. During this period, the northern margin of Tarim was relatively stable. During Jixian period, the whole area was relatively stable. Except for local folds and uplifts, most areas of Tianshan and Tarim are in a long-term stable sedimentary state. In the vast coastal and shallow sea environment, extremely thick magnesium-based carbonate rocks are generally deposited. The Altun Movement at the end of Jixian County had a wide influence. The Tarim margin began to fold and uplift. In the Sinian moraine conglomerate in Dongdashan, the apparent age 1080Ma in the biotite 40Ar/39Ar age spectrum of huge granite gravel reflects this movement. In Tianshan area, the tectonic movement is relatively strong, including not only metamorphism, but also magmatic intrusion and even crust-mantle differentiation.

The movement of Tarim occurred about 8 million years ago, especially in the northern margin of Tarim. A large number of age data show that strong regional metamorphism and migmatization occurred before 900 ~ 800 Ma. Then, in some areas, such as southern Zenger, it began to bulge. In Tianshan area, due to the influence of geological movement in the later period, especially the strong transformation of Hercynian movement, only the remains of this period were partially preserved. The movement of Tarim finally formed the pre-Sinian blocks of Tarim and Tianshan. Since then, the Sinian unconformity has covered the Qingbaikou system in the whole range. In Sinian, except for some areas in the northern margin of Tarim, it was in a uplift and denudation tectonic environment, and Tianshan and Altai areas were in a sedimentary metamorphic environment.

In Paleozoic, the formation and expansion of Junggar oceanic crust and the subduction of land blocks restricted the evolution and development of continental crust in northern Xinjiang. According to Pb-Pb isochron of sphene and feldspar of light gabbro and Sm-Nd isochron of gabbro in Tangbale ophiolite suite, the formation time of western Junggar oceanic crust began about 500Ma ago and lasted about 400Ma. Due to the gradual formation and expansion of the oceanic crust, and the continuous subduction of the Siberian plate to the north and the Tarim plate to the south, the continental crust in northern Xinjiang began to be active, in the process of repeated tension and compression, magma intrusion and frequent volcanic eruptions. According to the isotopic age data obtained in northern Xinjiang, a large number of age data have been obtained in the age ranges of 400Ma, 350Ma, 300Ma and 250Ma, and the peak value has been formed in the age statistical chart. At this stage, due to the collision between plates, the formation of deep faults and the mutual circulation of crust and mantle materials, some ore-forming elements are continuously brought into the crust from the mantle, and further evolved into enriched ores through magmatism in the crust. Therefore, the Late Paleozoic was the metallogenic period of precious and non-ferrous metals in Tianshan, Junggar and Altai. About 350 ~ 300 ma ago, due to the collision between plates, a new continent was formed and the three plates gradually merged into one. After Paleozoic, the northern margin of Tarim was in a relatively stable environment in the process of oscillation uplift. Therefore, it is beneficial to oil generation and storage, and the frequent orogeny in the northern Tianshan Mountains provides metallogenic conditions for metal minerals. After Permian, the whole northern Xinjiang showed an upward trend, gradually moving from the past turmoil to stability.

In Mesozoic and Cenozoic, the north-south compression made the tectonic activity active again. Some Indosinian and Yanshanian age data obtained by predecessors and this study in Altai region, especially some 40Ar/39Ar, Rb-Sr whole-rock isochron and zircon U-Pb dating methods, all indicate the existence of Mesozoic structure, metamorphism and mineralization, and there may be Mesozoic magmatic activity. In addition, the basalt in the northwest of Qinghe River was determined as Neogene by 40Ar/39Ar dating method, and its age was 18Ma (Hu Aiqin et al., 1994), which confirmed the existence of Cenozoic volcanic eruption in Altai area in northern Xinjiang.