Junggar Basin is one of the largest sedimentary basins in Northwest China. It is located in Xinjiang, and enclosed by the Tarbagata mountains of Kazakhstan on the northwest side, the Altai mountains of Mongolia in the northeast, and the Heavenly mountains (Tian Shan) in the South.
The geology of Junggar Basin mainly consists of sedimentary rocks underlain by igneous and metamorphic basement rocks. The basement of the basin was largely formed during the development of the Pangea supercontinent during complex tectonic events from Precambrian to late Paleozoic time. The basin developed as a series of foreland basins – in other words, basins developing immediately in front of growing mountain ranges – from Permian time to the Quaternary period. The basin's preserved sedimentary records show that the climate during the Mesozoic era was marked by a transition from humid to arid conditions as monsoonal climatic effects waned. The Junggar basin is rich in geological resources (e.g. petroleum, coal and ore deposits) due to effects of volcanism and sedimentary deposition.
- 1 Regional tectonic setting
- 2 Geology
- 3 Paleoclimate and environment
- 4 Tectonic evolution
- 5 Geological resources
- 6 See also
- 7 References
Regional tectonic settingEdit
The major structural components of the Junggar Basin divided into six parts:
- Wulungu Depression were formed by faulting and flat depression. There was about 2,000 – 4,000 m thick sedimentary layers that deposited from Permian to the present.
- Luliang uplift (Sangequan uplift) was surrounded by narrow but steeply dipping at the north and wide but gently dipping at the south. There were about 1,100 – 4,000 m thick sedimentary layers and the complete layer from Permian to the present can be found in the southern part. Also, the plunging fold was found in this area.
- Central Depression was formed by three major lowland plains where are in Manas, Central, and Wucaiwan. There were 5,000 m thick sedimentary layers from Carboniferous to Quaternary.
- West Uplift consists of Chepaizi-Paotai uplift and Urho-Karamay monocline.
- Chepaizi-Paotai uplift formed by eastward plunging fold with faulting. The footwall includes Jurassic-Quaternary sedimentary layers while the hanging wall consists of post-Carboniferous sedimentary layers.
- Urho-Karamay monocline was formed with thrust fault along the west-northwest boundary of the basin. The Indo-Australian plate collision during Neogene resulted in uplift of the northern Junggar basin. This also resulted in re-activation of Permian thrust faults, produced faults on basement rocks and rifting on basin margin to form Karamay-Urho monocline. This area concentrated abundant hydrocarbons on the anticline part.
- East Uplift (Zhangpenggou-Qitai uplift) was formed by deformations in several times. The formation of NE-trend plunging fold in this area activated the faulting of basement rocks.
- Tian Shan Foredeep formed during lower-middle Triassic since the Tian Shan has uplifted continuously. During Cretaceous, the basin sank again and thus water depth became shallow due to tectonic deformations. In Paleogene, the size of the lake kept reducing and the eastern basin become a landmass. Also, there was further subsidence of Tian Shan Foredeep because of the formation of Himalayan in Paleogene.
Basement rock of Junggar BasinEdit
In Precambrian section was made up of felsic-intermediate granite with the inclusion of greenstones and ophiolites, where the Paleozoic section consists of mainly potassium- and sodium-deficient extrusive rocks. The basalts in the basement which indicated trapped late Paleozoic oceanic crust that came from the mantle.
The sedimentary facies started to be dominant in Permian. The layers continuously deposited fluvial and lacustrine facies until the present day, mostly containing conglomerate, sandstone, siltstone, and mudstone.
|Rock unit (Distinct geological features)||Rock unit (Distinct geological features)||Rock unit (Distinct geological features)|
|Quaternary||Holocene||Terrestrial sediments with regional mud volcanoes and evaporite|
|Pleistocene||glacial tills and eolian loess & gravels|
(Dark-brown mudstone, siltstone & sandstone with thin conglomerate & limestone)
(Thickly-bed shale interbedded with sandstone & calcite grains)
(Shale with ostracods, dolomitic sandstone)
(Orange-red sandy mudstone)
(quartzose sandstone & mudstone)
(Green shale with marls)
(medium-grained sandstone & mudstone)
(Orange-red sandy shale)
(Mudstone at upper unit but conglomerate at lower unit)
(Sandy shale, siltstone, sandstone & conglomerate, some calcite nodules)
|Lower||Kalaza megasequence (99-154 Ma)
(Sandstone with marls, but mudstone and shale dominated in southern part. Conglomerate with cross-bedding structure at lowest unit. Presence of gypsum and fossil fish.)
|Shishugou megasequence (154-169 Ma)
(Sandy mudstone to sandstone, with calcite materials and dinosaur fossils.)
|Sangonghe megasequence (169-195 Ma)|
|Badaowan megasequence (195-206 Ma)|
(Yellow silty shale with some coal)
(Yellow conglomerate, sandstone, mudstone & shale)
(Greyish-green sandstone & mudstone)
(Conglomerate, sandstone with graded bedding)
(Red conglomerate, sandstone & mudstone)
(orange-red conglomerate with red mudstone)
(siltstone, sandstone & conglomerate)
(Greyish-green mudstone with sandstone, with some purple-red conglomerate and plant fossils)
(orange-red alluvial sandstone & conglomerate, with shale)
(Greyish-green feldspathic sandstone & mudstone, some fossiliferous limestone and black oil-shale)
(orange-red clastic sedimentary rocks)
(limestone with the presence of stromatolite)
(Grey mudstone, sandstone, conglomerate)
(Organe-red conglomerate, and fossil plant-bearing sandstone & volcanic flows)
(pyroclastic turbidite, locally thinly-bedded limestone)
(Conglomerate, Sandstone, calcareous shale)
(Grey tuff with regional limestone included brachiopod fossils, and pillow lava)
|Precambrian to Devonian||Basement rocks (various plutonic and volcanic rocks, ophiolites, turbidites tuffaceous and metasedimentary rocks)|
Paleoclimate and environmentEdit
Throughout Mesozoic, Junggar Basin was mainly in the fluvial and lake depositional environment.
The climate in the late Permian showed the fluctuation between dry- or wet-dominated climate. The pieces of evidence included the presence of both organic beds and red beds. In the early Triassic, reddish sedimentary rocks formed that indicated the dominance of semi-arid climate.
During Late Triassic-Early Jurassic, the Junggar basin was in a warm and wet climate due to the effect of continental monsoonal climate. From middle to late Jurassic, the climate shifted as a seasonal arid climate that initiated from the northeast and then widespread to the whole basin. This is because the Pangea started to break apart that halted the effect from the mega-monsoon system. Therefore, the basin became to be affected by westerlies. The westerlies contained the lesser moisture that has come from the northwest since the marine areas gradually minimized to the recent Caspian Sea. With the continuous uplift along the Tian Shan, the orographic effect around the basin intensifies the rain-shadow effect. The prominent rain-shadow effect results in a warmer seasonal arid climate in the basin. At the same time, the lakes in the basin had higher salinity and lower sedimentation influx.
Pre-Permian (before 290 Ma): basement rock evolutionEdit
Xinjiang paleocraton was pulled apart for a continental rifting episode to form extensional basins in Late Cambrian. The continuous divergence of the continental crust during late Cambrian to Ordovician shaped the West Junggar Ocean. The West Junggar Ocean presented as the present Tangbale and Honguleleng ophiolites from intra-plate volcanism, and then this volcanism shut in mid-upper Ordovician. The Ordovician first ocean basin indicated that eastern Junggar was over passive margin. Another rifting event established the Mayilashan ocean basin and back-arc basin in east Junggar during Silurian. However, the compressional environment restricted the two landforms so that they ended up shut and folded in the late Silurian. This eventually led to the convergence of Tarim, Kazakhstan and Siberian paleo-plates. They were from the original Xinjiang paleocraton that puzzled each other again.
Junggar Ocean and Kulumudi Ocean were produced from the third rifting event during lower-mid Devonian. Eventually, the Junggar ocean and Kulumudi Ocean moved towards the north and undergone the subduction from upper Devonian to Late-Carboniferous. At the same time, several volcanic arcs were developed during subduction. Three plates (Tarim, Kazakhstan, and Siberian) converged together to form a trapped ocean that surrounded volcanic arc and orogens in Mid-Carboniferous. Alkali-rich granites with gold deposits intruded the converged plates. This revealed the partial melting of the oceanic crust. This also marked as the last subduction event following the post-collisional stage in Late-Carboniferous. Besides, Such intrusive rocks demonstrated that this was the last melting episode of oceanic crust. As part of the Eurasian plate started to combine continental crusts for the three plates, to consolidate them as another modern stable continental block.
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.
Permian to Present (From 290 Ma): Junggar Basin evolutionEdit
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. This developed an alluvial-rich delta system around shallow lakes with the clastic sediments influx from uplifted Tian Shan and the northern part of the basin.
Junggar Basin contains the third-largest petroleum reservoirs in China. About two-third of oil can be found in the Karaamy-Urho monocline area. There was formed in Carboniferous deep-sea sedimentary rocks and lake sedimentary layers from Permian to Tertiary. For Carboniferous oil and gas deposits in this area, they were moved upward and accumulated in the Permian period and Mesozoic era sandstones. Then, the layers altered as the structural trap locations by tectonic activities in the later stage. Petroleum is dominant in Karamay, Baikouquan, Urho, Dushanzi, and Qigu. The oil and gas fields can be found on Tertiary Dushanzi sandstone. Besides, gas fields are found in the Karamay as well as the inland region of the basin.
Besides, Tian Shan Foredeep in the southern Junggar Basin (including Urumqi) is also available for the petroleum resources. The petroleum there were formed due to rapid subsidence, regional ductile with mobile intrusion, and cross-cutting on anticlines by orogenic activity (probably in Neogene) from the Tian Shan. Part of the oil-bearing sedimentary rocks was deposited in the salty oxygen-deficient lake environment during Permian. The crude oil in this sedimentary rocks formed by remains of algae and humus.
Bituminous coal was found in Tian Shan Foredeep. It was deposited in the lake or swamp environment in the Early to Middle Jurassic periods. For example, Badaowan, Sangonghe, and Xishanyao Formation. About 18 gigatonnes of coal can be recovered in Tian Shan Foredeep. Apart from Tian Shan Foredeep, the coal can be found in the base of alluvial fan and nearby the margin of lakes in the eastern and western margin of Junggar Basin.
- Porphyry Copper-gold deposits found in the west and northeast of the Junggar Basin.
- Iron deposits found in the eastern part of the basin due to early subduction events during Lower Carboniferous.
- During post-collision extensional events in Permian, gold deposits found on the west side and tin deposits found on the east side.
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