(China Petroleum Exploration and Development Research Institute, Beijing 100083)
According to the distribution law of pre-Sinian basement age and Sinian system, it is considered that the ancient Yangtze plate in Caledonian (Z-S) is larger than the Yangtze plate in today's narrow sense, including at least Songpan-Ganzi block and Qinling microplate, and belongs to the multi-island ocean system in the eastern part of the former Tethyan Ocean. According to the four stages of plate activity affecting the evolution of the craton basin, the Caledonian tectonic evolution of the Yangtze ancient craton can be divided into five stages, namely, the Sinian balance adjustment period, the Cambrian expansion period, the early and middle Ordovician convergence period, the middle and late Ordovician collision period and the Silurian new round balance adjustment period. Therefore, it can be inferred that there was a huge hydrocarbon generation center in eastern Sichuan-western Hunan-Hubei area in the early Paleozoic, and the ancient uplifts such as Leshan-Longnvsi Uplift, Jiangnan-Xuefeng Uplift and Qianzhong Uplift formed in Caledonian period were the direction areas for oil and gas migration in this period.
Key words: tectonic evolution of East Yangtze paleoplate in East Tethyan Caledonian
Tectonic evolution of ancient Yangtze plate in Caledonian
Wang Xinwei
(China Petrochemical Exploration and Production Research Institute, Beijing 100083)
Based on the study of pre-Sinian basement age and Sinian distribution, it is considered that the ancient Yangtze plate is larger than it is now, including at least Songpan-Ganzi block and Qinling microplate, and it was an integral part of the East Tethys Islands Ocean in Caledonian (from Sinian to Silurian in this paper). According to the four evolution stages of the craton basin affected by the movement between plates, the evolution of the ancient Yangtze Craton can be divided into five stages, namely, the balance adjustment stage of Sinian, the extension stage of Cambrian, the convergence stage of early and middle Ordovician, the collision stage of middle and late Ordovician and the new balance adjustment stage of Silurian. It can be inferred that there is a huge Paleozoic hydrocarbon-generating depression from eastern Sichuan to western Hunan and Hubei, and the ancient uplifts formed by Caledonian movement, such as Leshan-Longnvshi uplift, Jiangnan-Xuefeng uplift and central Guizhou uplift, are Caledonian oil and gas accumulation zones.
Keywords Caledonian tectonic evolution of the ancient Yangtze plate in East Tethyan
In a narrow sense, the Yangtze plate is bounded by Jiashan-Xiangshui fault and Mianlue-Dabie Mountain southern margin fault in the north, separated from Songpan-Ganzi block and Changdu block by Longmenshan fault and Jinshajiang-Ailaoshan fault in the west, and adjacent to Huaxia plate by Jiangshaogu suture zone in the southeast (figure 1). Yangtze Plate is the main field of oil and gas exploration in southern China. For a long time, geologists in China have done a lot of research work, but most of them have focused on the study of residual basins transformed by tectonic evolution, sequence framework and late tectonic movement [1 ~ 4], and there is still a lack of research on the development characteristics of the middle Yangtze ancient plate in Caledonian craton basin and its relationship with the original Tethys Ocean. Based on the previous research results, this paper analyzes the Caledonian tectonic evolution of the Yangtze ancient craton and its relationship with the original Tethys Ocean according to the stages of plate activity that affected the evolution of the craton basin, and focuses on the nature and distribution characteristics of the Silurian prototype basin.
Figure 1 Schematic Diagram of the Range of the Ancient Yangtze Plate
(modified according to reference [2])
1 basement structure and paleoplate range
The basement of the Yangtze plate refers to the strata before the Neoproterozoic Sinian system, which has a double-layer structure [5]. The lower structural layer is Archean U-Pb Proterozoic crystalline basement, which is a set of deep metamorphic rocks (metamorphic degree reaches amphibolite facies) composed of intermediate-basic volcanic rocks and pyroclastic rocks, and strong basic-ultrabasic rock intrusions, which are called Kangding complex (Kangdian area, 1760 ~ 3 100 Ma) and Jidong complex respectively. The upper structural layer is Mesoproterozoic shallow metamorphic rock series, and the metamorphic degree is greenschist facies. The protoliths are a set of deep and shallow marine clastic rocks, pyroclastic turbidites, pillow tholeiite, siliceous rocks and carbonate rocks, which are called Kunyang Group (Kangdian District, 1002Ma), Huangshuihe Group (West Sichuan), Huodiya Group (North Sichuan), Shennongjia Group (Sichuan and Hubei) and Fanjingshan Group (Sichuan and Guizhou) respectively.
The Sinian system is the first set of sedimentary caprocks when the Yangtze plate entered the platform stage. According to the distribution law of basement age and Sinian system, many scholars believe that the scope of the ancient Yangtze plate is much larger than that of the narrow Yangtze plate, which may include Songpan-Ganzi block and Qinling microplate. The main evidences are:
(1) In Wenxian-Qingchuan area on the east side of Songpan-Ganzi block, a large area of bedrock block consisting of Mesoproterozoic deep metamorphic Bikou Group is exposed, and its two wings are covered by Dengying Formation, so it can be inferred that Dengying Formation should be connected with the basement of Sichuan Basin when deposited [6].
(2) There are coarse-grained terrigenous clastic rocks in the Lower Sinian Baiyigou Group in the east of Jiangzha, South Qinling. The sediment particles are coarse in the south and fine in the north, and the gravel decreases from south to north. There are three isotopic ages of terrigenous gravels and fine clastic rocks, namely, about 2000Ma (tuff), 1000 ~ 1400 Ma (granite) and about 740Ma (rhyolite).
(3) The bedrock blocks in the southeast of Songpan-Ganzi block are all products of Jinning tectonic magmatism, such as Danbagezong granite (1585Ma, detrital zircon 207Pb/206Pb), Shapingguan granite (1kloc-0/7 Ma, zircon U-Pb method) and Xingwenping granite.
(4) The Qinling microplate has a double-layered pre-Sinian basement of the Yangtze plate, namely Archean-Proterozoic crystalline basement and Mesoproterozoic-Neoproterozoic transitional metamorphic basement. The metamorphic degree of the lower basement has reached intermediate-deep metamorphic amphibolite facies-granulite facies, and Foping complex and Xiaomoling and Douling complexes are mainly exposed. The metamorphic degree of the upper basement is mostly shallow metamorphic greenschist facies, which is a set of meso-Neoproterozoic sedimentary-volcanic rock series dominated by volcanic rocks, including Liaoxi Group (965 ~ 1304 Ma) and Gulinghe Group (71~10/kloc-0) respectively. The Lower Sinian is generally absent in the Qinling area, while the Doushantuo Formation and Dengying Formation of the Upper Sinian are widely developed in the southern Qinling area, without crossing the Shangdan line northward, indicating that the Qinling microplate belongs to the Yangtze ancient plate, and the Yangtze ancient plate and the North China ancient plate were separated in the early Sinian [8].
It can be inferred from the above evidence that the range of the Yangtze ancient plate at least includes the Songpan-Ganzi block and the Qinling microplate, which together constitute a large-scale Yangtze ancient craton (Figure 1).
2 the relationship with the original Tethyan Ocean
The Jinning movement, which occurred at the end of the Neoproterozoic Qingbaikou period, formed the folded basement of the Yangtze ancient plate, and its motive force was not only related to the collision and splicing of the Cathaysian block and the Yangtze block along the Yanshou fault (suture) zone, but also related to the collision and splicing of the Yangtze ancient plate and the North China ancient plate along the Shangdan suture zone at that time [2]. Huang et al. [9] thought that Jinning Movement (called Tarim Movement in Tarim Basin) formed a complete China platform, and called it the ancient China platform. After the extension from Sinian to Early Cambrian, the ancient China platform disintegrated to form Qilian Ocean and Qinling Ocean. Li et al. [10] called the extension movement at this time "Xingkai ground fissure movement". The convergence of Jinning period and the extensional environment at the beginning of Sinian in Chinese mainland may be global, belonging to the formation of Neoproterozoic Rodinia Pangea and the disintegration of Pangea from the end of Precambrian to the beginning of Early Paleozoic [1 1 ~ 12]. After the disintegration of Pan-continent, the original Gondwana continent and Lauya continent were formed, as well as the Chinese, Yangtze-Cathaysian, Qiangtang-Changdu, Indo-China Peninsula, Tarim and Qaidam landmasses and micro-landmasses scattered in the original Tethyan Ocean (the time limit is Sinian-Early Paleozoic). Li Xingzhen et al. [13] divided the original Tethys Ocean into four branches according to the spatial distribution of the continental suture zone, namely, the ancient Asia-South Tianshan Ocean in the north, the Kunyang Ocean in the middle and the ancient Jinsha River-Ailao Mountain Ocean and the ancient Lancang River Ocean in the south (Figure 2). These oceans are connected with the ancient Tethys in West Asia and Europe to the west, belonging to the category of primitive Tethys. At the same time, the residual basins in South China extended again from Sinian, separating the Yangtze ancient plate from the Cathaysian plate and connecting it with the ancient Jinsha River-Ailaoshan Ocean to the south. Engel Wusu Ocean (also called Gould Yang Kim) developed in Alashan region may connect the ancient Asian Ocean with the Qin, Qi and Kun oceans. Therefore, the Sinian-Early Paleozoic Yangtze ancient plate belongs to the original Tethys island ocean system, and its structural evolution is closely related to the structural evolution of the North China plate and the Cathaysian plate on both sides and the transformation from the original Tethys ocean to the Paleo-Tethys ocean.
Fig. 2 Schematic diagram of ocean distribution in East Tethys Island
(modified according to reference [13])
(1) Paleo-Asian oceanic suture zone; (2) Chyi Chin Kunyang suture zone; (3) Ancient Jinsha River-Ailaoshanyang suture zone; (4) Ancient Lancang-Dayang suture zone; (5) Engel Wusu suture zone; (6) South China limited ocean basin suture zone
3 Caledonian tectonic evolution
The Yangtze ancient plate has evolved into a craton basin since Sinian. The interaction between plate tectonics and the effective range of internal stress in the floor of craton basin is the main controlling factor affecting the evolution of craton basin [14]. Plate activities affecting the evolution of the craton basin can generally be divided into four stages, namely: ① in the expansion stage, the craton is characterized by the development of rift system and graben or depression trough, and rifting and rapid deposition occur simultaneously; (2) The convergence stage is generally accompanied by the formation of pre-arc and post-arc basins, and at the same time, the weak compressive flexural basins of foreland and craton are formed; (3) In the collision stage, the basin tilted due to the compressive stress caused by the continental-continental collision (A-type subduction) and the intracontinental collision (C-type subduction), and the lithosphere at the edge of the craton was bent due to the tectonic load of the collision zone, thus forming a pattern in which foreland basins and intracontinental basins appeared in pairs for a long time. At the same time, the compressive stress can be transmitted to the deep part of the craton, causing the deformation of structural weak zones (such as ancient cracks and suture lines) in the early crust. (4) During the termination and balance adjustment period, with the shortening and thickening of the earth's crust and the fixation of giant suture lines, the continent or a part of the continent rose above sea level and suffered extensive erosion, resulting in major sedimentary discontinuity; At the same time and later, due to the erosion of tectonic load in collision zone and the settlement of deep lithospheric plate, the orogenic belt collapsed, which led to the rebound of crustal balance and the increase of regional tilt. When the new stress field appears, the plate structure will produce a new range of activities, and the craton basin will enter a new round of evolution cycle. In most cases, the main sequence boundary in craton basin is unconformity, which reflects the main period of plate movement direction and movement rate change, and the new stress field changes the shape and direction of future basin formation. Therefore, according to the tectonic cycle of the evolution of the craton basin, this paper divides the Caledonian tectonic evolution of the Yangtze ancient craton into five stages, namely, the Sinian balance adjustment period, the Cambrian expansion period, the early and middle Ordovician convergence period, the middle and late Ordovician collision period and the Silurian new round balance adjustment period (Figure 3).
Fig. 3 Schematic diagram of Caledonian tectonic evolution of Yangtze ancient craton
3. 1 sinian balance adjustment period
After the violent plate collision and assembly at the end of Jinning, with the denudation-unloading at the top of the orogenic belt and the subsidence-rooting of the lithosphere at the bottom, the post-orogenic extension and collapse occurred, and the Sinian Yangtze ancient plate entered a period of balance adjustment, including two stages: the early Sinian intracontinental rift and the late Sinian post-fracture depression (Figure 3(a)).
The rifting of the Yangtze ancient plate and its periphery in the early Sinian is mainly manifested as follows: ① On the northern margin of the Yangtze ancient plate, the North China plate stitched with the Yangtze plate in the late Jinning period began to pull apart again in Sinian, leading to the formation of Qin Qiyang, and the ophiolite melange in the Fengdan Group in the northern Qinling area showed a complete evolution cycle of rift-small ocean basin-active continental margin; ② Volcanic rocks of Suxiong Formation are developed in Ganluo area on the northwest margin of Yangtze ancient plate; ③ Asbestos-Chengjiang Rift Zone was formed in the west of Yangtze landmass, in which continental volcanic-sedimentary rock series of Lower Sinian system with huge thickness (3 ~ 6 km) were accumulated; (4) In Jinning period, the South China Rift System was developed on the basis of the South China Basin between the southern margin of Yangtze Plate and the northern margin of Huaxia Plate, namely, the Guixiang Submarginal Rift Basin (the southern margin of Yangtze Plate) and the Jiangxi-Guangdong Submarginal Rift Basin (the northern margin of Huaxia Plate), both of which deposited a sub-deep-sea clastic rock assemblage with a thickness of about 3 ~ 6 km. The northern boundary of Gui Xiang Rift Basin is roughly equivalent to the present Jiangnan-Jiuling-Xuefeng Uplift Belt ⑤ except the extensional depression basin and the middle and lower reaches of the Yangtze River.
With the strengthening of extension in late Sinian, it evolved into post-split depression deposits. The whole Yangtze ancient plate was submerged by seawater and became a typical intra-craton basin, which widely accepted carbonate deposits in shallow sea of platform facies. The unconformity between the upper and lower Sinian is a separation unconformity formed by the transformation from rift basin to depression basin [14], which is limited to the distribution area of rift basin.
3.2 Cambrian expansion period
After the balance adjustment of Sinian system, the Cambrian Yangtze ancient craton entered the expansion period (Figure 3(b)). At this time, Cambrian-Ordovician ophiolite developed in many places around the Yangtze ancient plate in North Qilian Mountain, reflecting that the typical oceanic crust (Qilian Ocean) was pulled out in Cambrian-Ordovician in North Qilian Mountain. The Jinsha River-Lancangjiang Rift in the southwest began to expand, which led to the separation of the Changdu-Simao block from the Yangtze ancient plate. The south China rift system in the southeast has further expanded into the south China rift ocean basin, and a set of deep-water sedimentary formations of siliceous rocks, black shales and turbidites have developed. Within the Yangtze ancient craton, there are rift troughs in the post-Longmenshan area, and a set of shallow-sea clastic rocks are deposited. Aola trough (volcanic rock of Erdaoqiao Formation of Upper Cambrian) extends in Ankang-Ziyang-Zhuxi area of South Qinling, and shallow-water facies-slope facies carbonate rocks are deposited in the south of Aola trough. The marginal basins of Gui Xiang Craton in the southern margin of Yangtze Paleocraton and Chuzhou Craton in the eastern part of Tanlu Fault belong to continental slope or low slope deep basin environment. In today's middle-upper Yangtze region, characterized by extensional depression deposits in craton, the maximum transgression amplitude was reached in the early Early Cambrian (the sedimentary period of Meishucun-Qianzhusi Formation), and black shale and phosphorite were widely deposited, becoming the main source rocks of Lower Paleozoic; In the middle of Early Cambrian (Canglang period), the subsidence mechanism of the basin changed from extension to thermal subsidence, and the geomorphic pattern disappeared. With the increase of sedimentation rate, the sea level drops and the seawater becomes shallow. By the Middle Cambrian, it evolved into tidal flat facies and limited platform facies mudstone and dolomite deposits, and gypsum salt rock deposition environment appeared [15]. In the Late Cambrian, regression continued, which was generally carbonate deposits in coastal shallow seas with limited platform facies.
3.3 Early-Middle Ordovician convergence stage
The Yunan movement between Cambrian and Ordovician marked the convergence of the Yangtze ancient plate from the early Ordovician (Figure 3(c)). On the south side of the Yangtze ancient plate, the South China rifted ocean basin dived southeast along the northwest of Wuyi-Yunkai belt, which led to the uplift of Yunkai area, island arc volcanic activity and migmatization in Wuyi-Yunkai belt (Ordovician-Silurian did not have this phenomenon), and the lower-middle Ordovician flysch clastic rock formation in Yunkaishan area was slightly unconformity covered with Cambrian and lower-middle Ordovician in Baihuangling area of Guangxi. On the north side of the Yangtze ancient plate, Qin Qiyang converged and contracted, and the Yangtze plate subducted under the North China plate, which led to the transformation of the passive continental margin of the early southern margin of the North China plate to the active continental margin, forming a complete trench-arc-basin system. The location of the main subduction zone should be the Shangdan suture zone, and the "bimodal" volcanic rocks (up to 3000 meters thick) of the Huoshenmiao Formation of Erlangping Group in the northern part of the back-arc basin are typical, representing early back-arc extension. In the Yangtze ancient plate, it is characterized by weak compressional depression deposits in craton, and its lithology is mainly platform facies shallow sea carbonate rocks and argillaceous rocks. At this time, the Jiangnan-Xuefeng belt may be underwater low uplift.
3.4 Late Middle Ordovician-Late Ordovician collision stage
From the late Middle Ordovician to the late Ordovician, with the closure of the South China rifted ocean basin and Chyi Chin Ocean, the Yangtze ancient plate entered the collision stage (Figure 3(d)). The molasses of Jianling Formation of Middle Ordovician in Yaxian area of Hainan Island is in angular unconformity contact with shale of Shatang Formation (Figure 4), indicating the initial time of tectonic movement in this period. The main body of the whole North China plate was affected by the subduction of the southern Qin Qiyang and the northern ancient Asian Ocean, showing overall uplift and erosion, thus missing the upper Ordovician-Devonian deposits; South Qinling, Houlongmen Mountain, Yunnan, Guizhou and Guangxi all rose to land, but the upper part of Middle Ordovician was missing. The coastal areas of Zhejiang and Fujian were uplifted into mountains due to the collision between the Yangtze ancient plate and the Cathaysian plate, and at the same time, a late Ordovician foreland basin was formed in western Zhejiang, accumulating a set of shallow water and land debris flysch; The residual trough formed by the right-lateral shear collision between Cathaysian plate and Yangtze ancient plate in Qin Fang area continues to be deposited in deep-water basin; The hinterland of the Yangtze ancient craton is a compressional depression basin, which has deposited a set of carbonate rocks from shallow sea to deep sea. With the intensification of compression, the basin area decreased, the ancient land expanded and transformed into shelf facies clastic rock deposits. At the end of the late Ordovician, the strong Caledonian movement closed the Guqin trench, and the strata in South China were squeezed and deformed, forming the Caledonian fold belt. In the Yangtze ancient craton, the structural patterns of "big uplift and big depression" such as Jiangnan uplift, Qianzhong uplift, Leshan-Longnvsi uplift and Ningchao Tailong were formed, which became the direction of oil and gas migration in Caledonian.
Fig. 4 Schematic diagram of unconformity between Jianling Formation (O2j) and Shatang Formation (O2s) of Middle Ordovician in Yulin Port, Ya County, Hainan Province [16]
1- Quaternary caprock; 2- calcium siliceous composite conglomerate; 3- shale; 4— Gravel limestone; 5-Limestone
3.5 Silurian balance adjustment period
After entering the Silurian, the collision ended, the compressive stress relaxed, and the crust rebounded evenly, thus developing post-orogenic rifting and making the Yangtze ancient craton enter a new evolution cycle (Figure 3(e)). The aulacogen [17] was formed by the extension and rifting of the North China plate and the Yangtze paleoplate along the Mianwei line, which is mainly marked by the deep-water deposits and volcanic deposits of the Silurian Baishuijiang Formation on the north side of Mianwei line, as well as the "bimodal" volcanic rocks and alkaline volcanic rocks, argillaceous rocks and siliceous rocks of the Silurian Donghe Formation in Dabashan area. In addition, there are long and narrow deep-water turbidite deposits such as Bailongjiang Group in the western Qinling Mountains and Maoxian Group in Houlongmen Mountain on the western margin of Yangtze ancient plate. On its southeast edge, the crust was pulled back along the Qin Fang line, forming a regenerative rift trough. A set of slump turbidite series consisting of coarse sandstone, gravel sandstone and conglomerate developed at the bottom of Lingshan Formation of Lower Silurian, which was unconformity superimposed on the middle-upper Ordovician. Accordingly, the upper Yangtze region is characterized by weak extensional depression deposits in craton, which are mainly composed of shallow-sea carbonate rocks and clastic rocks.
During the Silurian balance adjustment period, the Yangtze ancient plate produced a lower degree of crustal extension than Sinian, indicating that most rift zones did not develop "bimodal" volcanic rocks, but only developed extensional slump-type deep-water turbidites, which may be related to the stronger orogeny at the end of Jinning than at the end of Late Ordovician. After Silurian balanced adjustment, the Yangtze paleoplate entered a new stage of craton basin evolution such as expansion, convergence and collision. At the same time, with the formation and expansion of Mianlueyang, Changning-Mengningyang, Jinsha River, Ganzi-Litang and Babuyang in Hercynian [2], East Tethys completed the transformation from the original Tethys island ocean system to the Paleo-Tethys island ocean system.
In addition, based on the Caledonian tectonic evolution of the Yangtze ancient plate, it can be seen that the eastern Sichuan-western Hunan-Hubei region has always been the sedimentary center of the basin in the craton, and a huge hydrocarbon-generating depression has developed. Paleo-uplift formed in Caledonian period, such as Leshan-Longnvsi uplift, Jiangnan-Xuefeng uplift and Qianzhong uplift, are the direction areas of oil and gas migration in this period.
4 conclusion
(1) The age of the pre-Sinian basement and the distribution of the Sinian system show that the Caledonian (Z-S) range of the Yangtze ancient plate is larger than that of the Yangtze plate in the narrow sense now, including at least the Songpan-Ganzi block and the Qinling microplate, and the North China plate, the Qaidam plate, the Tarim plate, the Cathaysian plate, the ancient Asian ocean, the Qin-Qi-Kun ocean and the ancient Jinsha River-Ailaoshan ocean.
(2) According to the four stages of plate activity affecting the evolution of the craton basin, the Caledonian tectonic evolution of the Yangtze ancient craton can be divided into five stages, namely, Sinian balance adjustment period, Cambrian expansion period, early-middle Ordovician convergence period, middle-late Ordovician collision period and Silurian new round balance adjustment period.
(3) In the early Paleozoic, there was a huge hydrocarbon generation center in the eastern Sichuan-western Hunan-Hubei area, and the paleo-uplift formed in Caledonian period, such as Leshan-Longnvsi uplift, Xuefeng uplift and central Guizhou uplift, was the direction of oil and gas migration in this period.
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