The Jingyihuo railway ( Chinese : 精伊霍铁路 ; pinyin : Jīng yī huò tiělù ), short for Jinghe–Yining–Khorgas railway , is the first electrified railway in operation in Xinjiang, China. The line is 286 km in length and connects Jinghe , Yining and Khorgos . The Jingyihuo railway branches from the Northern Xinjiang railway at Jinghe in the Junggar Basin and heads south through the Tian Shan range into the Ili River Valley. Cities and towns along route include Jinghe, Nilka County , Yining County , Yining , Huocheng County and Khorgos, on the border with Kazakhstan .
35-633: The line opened to trial operation in December 2009. Passenger train service to the Yining railway station ( 43°58′00″N 81°16′30″E / 43.96667°N 81.27500°E / 43.96667; 81.27500 ) began in July 2010. One of the three daily Ürümqi-Yining passenger trains (all running overnight) was extended to Khorgos in December 2013. On its way from the Dzungarian Basin (where
70-467: A felsic rock is given according to the TAS classification of Le Maitre (1975). However, this only applies to volcanic rocks. If the rock is analyzed and found to be felsic but is metamorphic and has no definite volcanic protolith , it may be sufficient to simply call it a 'felsic schist'. There are examples known of highly sheared granites which can be mistaken for rhyolites. For phaneritic felsic rocks,
105-455: A tridimensional network of SiO 4 tetrahedra connected to each other. Once released in water and hydrolyzed, these silica entities can indeed form silicic acid in aqueous solution. The term "felsic" is a derivation of the words " fel dspar" and " si lica". The similarity of the resulting term felsic to the German felsig , "rocky" (from Fels , "rock"), is accidental. Feldspar is from
140-472: 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 affected by westerlies . The westerlies contained
175-420: Is granite . Common felsic minerals include quartz, muscovite , orthoclase , and the sodium-rich plagioclase feldspars ( albite -rich). In modern usage, the term acid rock , although sometimes used as a synonym, normally now refers specifically to a high-silica-content (greater than 63% SiO 2 by weight) volcanic rock , such as rhyolite . Older, broader usage is now considered archaic. That usage, with
210-460: Is a petrologic field term used to refer to very fine-grained or aphanitic , light-colored volcanic rocks which might be later reclassified after a more detailed microscopic or chemical analysis. In some cases, felsic volcanic rocks may contain phenocrysts of mafic minerals, usually hornblende , pyroxene or a feldspar mineral, and may need to be named after their phenocryst mineral, such as 'hornblende-bearing felsite'. The chemical name of
245-550: Is contrasted with mafic rocks, which are richer in magnesium and iron . Felsic refers to silicate minerals , magma , and rocks which are enriched in the lighter elements such as silicon , oxygen , aluminium , sodium , and potassium . Molten felsic magma and lava is more viscous than molten mafic magma and lava. Felsic magmas and lavas have lower temperatures of melting and solidification than mafic magmas and lavas. Felsic rocks are usually light in color and have specific gravities less than 3. The most common felsic rock
280-700: 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
315-687: The Altynkol railway station on the Kazakh side of the border opposite Khorgos opened in September 2012. The railway border crossing (freight port of entry ) at Khorgos became operational in December 2012. This People's Republic of China rail-related article is a stub . You can help Misplaced Pages by expanding it . Junggar Basin The Junggar Basin ( simplified Chinese : 准噶尔盆地 ; traditional Chinese : 準噶爾盆地 ), also known as
350-817: The Dzungarian Basin or Zungarian Basin , is one of the largest sedimentary basins in Northwest China . It is located in Dzungaria in northern Xinjiang , and enclosed by the Tarbagatai Mountains of Kazakhstan in the northwest, 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
385-605: The German Feldspat , a compound of the German Feld , meaning field, plus spat[h] , meaning mineral. In order for a rock (rather than a mineral ) to be classified as felsic, it generally needs to contain more than 75% felsic minerals (namely quartz, orthoclase and plagioclase ). Rocks with greater than 90% felsic minerals can also be called leucocratic , from the Greek words for white and dominance. Felsite
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#1732780922947420-590: The Karamay-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
455-882: The Northern Xinjiang railway runs) to the Ili Valley (where Yining is), the railway crosses the Borohoro Mountain Range (one of the ranges of the Tian Shan ) in the 13-km long North Tianshan Tunnel ( Chinese : 北天山隧道 ; pinyin : Běi tiānshān suìdào ). The Jinghe–Yining section is electrified. In December 2011, a 293-km railway on the Kazakhstan side of the border connected the Khorgos border crossing to Zhetigen terminal (near Almaty ). A regular passenger service between Almaty and
490-708: 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,
525-467: 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. Major stratigraphic units in the Junggar basin from Carboniferous are shown in ascending order in
560-458: 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
595-523: 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
630-486: 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. According to Guinness World Records it is a land location remotest from open sea with great-circle distance of 2,648 km (1,645 miles) from
665-615: 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. Ore deposits in the Junggar Basin were mainly formed in the Paleozoic era which was related to tectonic development. The followings are the available ore deposits in Junggar Basin: Felsic In geology , felsic is a modifier describing igneous rocks that are relatively rich in elements that form feldspar and quartz . It
700-458: The contrasting term "basic rock" (MgO, FeO, mafic ), was based on an ancient concept, dating from the 19th century, that " silicic acid " (H 4 SiO 4 or Si(OH) 4 ) was the chief form of silicon occurring in siliceous rocks. Although this intuition makes sense from an acid-base perspective in aquatic chemistry considering water-rock interactions and silica dissolution, siliceous rocks are not formed by this protonated monomeric species, but by
735-780: 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
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#1732780922947770-399: 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
805-895: The following table: (Dark-brown mudstone, siltstone & sandstone with thin conglomerate & limestone) (Thickly-bed shale interbedded with sandstone & calcite grains) (Mudstone, sandstone) (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) (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.) (Sandy mudstone to sandstone, with calcite materials and dinosaur fossils.) (Presence of mudcracks in lower unit, coal red beds and dinosaur tracks at
840-472: 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
875-460: 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. Xinjiang paleocraton
910-463: 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
945-498: The nearest open sea at 46°16′8″N 86°40′2″E / 46.26889°N 86.66722°E / 46.26889; 86.66722 ( Land farthest from sea ) . The major structural components of the Junggar Basin divided into six parts: 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
980-399: 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) Throughout Mesozoic, Junggar Basin was mainly in
1015-400: 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
1050-477: 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 ,
1085-558: 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
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1120-534: 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-thirds of oil can be found in
1155-903: The top unit. Petrified woods were preserved. ) (Conglomerates in southern and eastern part. Massive mudstone beds and soft-sediment deformation in northwest. Widespread coals were present. Petrified woods and plant fossils were preserved. ) (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
1190-562: 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
1225-584: 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
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