Figure
1.
Basin distribution in the China seas and its adjacent areas (according to Zhang et al., 2010, 2016).
| Citation: | Xin’gang Luo, Wanyin Wang, Ying Chen, Zhizhao Bai, Dingding Wang, Tao He, Yimi Zhang, Ruiyun Ma. Study on the distribution characteristics of faults and their control over petroliferous basins in the China seas and its adjacent areas[J]. Acta Oceanologica Sinica, 2023, 42(3): 227-242. doi: 10.1007/s13131-022-2138-6
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Oil and gas resources play an increasingly important role in economic development. With the development of the oil and gas energy exploitation, the exploration of oil and gas resources in China has progressively march toward deep strata and deepwater areas. However, the geological conditions of deep strata and deepwater areas are overly complex, hindering resource explorations. How to accurately predict the distribution of deep oil and gas reservoirs is an important challenge and practical to be solved. Deep and large faults play a key role in hydrocarbon accumulation and can be used to predict oil and gas reservoirs. In this paper, we focused on the China seas and its adjacent areas (Fig. 1), which located at the east of Eurasia and west of the Pacific. The study area is an extension of a very long and broad tectonic active belt, including lands in eastern China (the eastern area of the Central Asian orogenic belt, North China Block, and South China Block) and seas (the Bohai Sea, the Yellow Sea, the East China Sea, and South China Sea).
Faults are abundant in the Bohai Sea area and its adjacent continental margin. Since the late Paleozoic, the North China Plate where the Bohai Sea is located has been successively affected by the northern Siberia Plate, the southern Yangtze Plate, the Indian Plate, and the eastern Pacific Plate, resulting in deep mantle movement and extremely active strike-slip faults. The superposition of the two tectonic systems, the Indosinian NWW−EW trend and the Yanshanian NNE trend of the Mesozoic, formed the basement tectonic pattern of the east−west zone and the north−south block in the Bohai Sea (Zhai et al., 2004). The Yellow Sea and its surrounding areas are mainly controlled by NNE- and NE-trending faults, and the dominant faults in the basin are also NNE−NE-trending, which have a large extension length and divide secondary structural units in the basin. A large number of small NNE-, NWW-, and EW-trending faults exist between the dominant faults and often appear in the shape of an echelon, controlling secondary depressions in the basin. The East China Sea and its adjacent areas are mainly composed of NE-to-NNE-, NW-, and nearly EW-trending faults, including tensional normal faults, compressional thrust faults, and shear-translational faults (Liu, 1992; Li, 2008). The South China Sea and its adjacent areas have complex structures and multiple fault types, which consist of NE−NEE-, NW-, and near-SN-trending faults. The dynamic characteristics are tensile in the north, compressional in the south, shear in the west, and subduction in the east, forming a tectonic pattern of “north−south zoning and east−west block” (Song et al., 2002; Lu et al., 2015; Luo et al., 2018). Based on the previous fracture research results (Liu, 1986; Hall, 2002; Chen et al., 2005; Lin et al., 2009; Xu et al., 2010; An et al., 2012; Dai et al., 2018; Wu et al., 2013, 2020; Luo et al., 2018; Liu, 2018; Zheng et al., 2019; Zhang et al., 2020; Qin et al., 2020). The main faults are NE-, NW-, and SN-trending, and the deep-large faults mainly include the Tan-Lu fault, Jiangshao fault, Okinawa Trough fault, Yushanjiumi fault, the coast fault in the northern South China Sea, Mesozoic Subduction fault in the north of the South China Sea, Xisha Trough fault, Zhongnan-liyue fault, Red River fault, Majiang-Heishuihe fault, Lupar fault, the west margin fault of the South China Sea, Manila trench fault, the southern margin fault of the Nansha Trough, Palawan-Sabah faullt, etc. in the China seas and its adjacent areas (Fig. 2). According to the cutting depth, faults can be divided into ultra-crustal faults and crustal faults (Zhang, 2008). The deep-large faults mentioned above are ultra-crustal faults. Crustal faults are widely developed in every basin in the study area, and their strikes are inherited or controlled by ultra-crustal faults.
Oil and gas resources in the China seas and its adjacent areas are distributed mainly in land and sea basins. At present, the proven continental petrol-bearing basins lie in the north of the Qinling-Dabie orogenic belt, and only a few basins (Sichuan Basin, Chuxiong Basin, and Lanping-Simao Basin) are distributed in the south. Marine petroliferous basins are mainly distributed in marginal seas, and the amount of oil and gas resources greatly varies among different basins (Xie and Gao, 2020), making oil and gas explorations even more challenging. Faults, as one of the main factors causing this difference, have been extensively studied. Hydrocarbon accumulation has been investigated on well-known active faults worldwide, such as the San Andreas active fault belt, the North Anatolia active fault, the Philippine active fault, the Japan Median Tectonic Line active fault, the Alpine active fault belt, Wasarch active fault belt, Talas Fergana active fault system, Altun active fault zone, and Tan-Lu fault (Stewart and Poole, 1975; Zhu et al., 2004, 2009b; Makino et al., 2007; Tsutsumi and Perez, 2013). Regarding hydrocarbon accumulation on active faults, it was found that active faults play a dual role in the formation and destruction of oil and gas reservoirs, and fault sealing is the main reason for the disparity in the enrichment degree of reservoirs. Multi-stage migration and accumulation of oil and gas along faults constitutes the main form of episodic hydrocarbon accumulation in active faults. Activities in the late stage of a fault inevitably destroy early oil and gas reservoirs. Therefore, the investigation of the accumulation and destruction of oil and gas reservoirs by fault activities, especially by the strongly active tectonic belt with a multi-stage tectonic cycle and multiple stress backgrounds, is a great challenge (Lv, 2012).
In short, the previous studies on the faults in China seas and its adjacent areas have been conducted independently in each sea area, and there are few studies on plane position and apparent depth inversion of faults in large area. According to previous fracture results, the plane position and extension direction of ultra-crustal faults are basically consistent, but the crustal faults are less studied. In addition, an understanding of the relationship between faults and reservoir distribution has remained obscure. In this work, the gravity anomaly, its normalized vertical derivative of the total horizontal derivative (NVDR-THDR), and gravity and magnetic anomaly fusion results were used to study the plane distribution characteristics of major faults in the China seas and its adjacent areas, and the Tilt-Euler method (Salem et al., 2008) was used to study the vertical apparent depth characteristics of the faults. Based on the inferred faults, gravity and magnetic anomaly processing data, and geological structures, we put forward the concept of influence factor of faults for the first time. According to this factor, we studied how faults control petroliferous basins in the China seas and its adjacent areas and predicted key areas for oil and gas exploration. Our findings can provide new insights into oil and gas exploration, mineral resource exploration, and deep geological structure research in the China seas and its adjacent areas.
Due to the location of this study area at the intersection of the Pacific Plate, Eurasian Plate, and Indo-Australian Plate, the spectacular trench-arc-basin system and complex oceanic and continental tectonic patterns were shaped (Li et al., 2017, 2019; Qin et al., 2020). The continental margin of the study area is composed of the eastern continental margin and the southern continental margin of China, which differ in terms of tectonic framework and evolution. The eastern continental margin includes the Bohai Sea, Yellow Sea, and the East China Sea, which are mainly influenced by the convergence of the Pacific Plate and the Eurasian Plate (Zhang, 2008). The southern continental margin, which includes the South China Sea and the Philippine Island arc, is affected not only by the Eurasian Plate and the Pacific Plate but also by the Indo-Australian Plate. It is controlled by the relative movements and interactions of the three plates, leading to structural complexity. Therefore, faults and petroliferous basins have concentrated in the whole China seas and its adjacent areas. The land area from north to south is Siberian block, Central Asian Orogenic belt, North China Block and Yangtze-South China Block. The sea area from west to east is the China seas area (Bohai Sea, Yellow Sea, East China Sea and South China Sea), East Asian Continental Margin convergence zone and Philippine Plate (Fig. 3). The complexity of the structure in the study area leads to a large number of faults (Hall, 2002; Wu et al., 2013; Luo et al., 2018; Zheng et al., 2019; Qin et al., 2020), and the fault distribution is closely related to the distribution of oil and gas. Therefore, it is very important to study the distribution of faults in this area and its relationship with oil and gas basins for oil and gas prediction.
The satellite altimetry gravity anomaly data are from the Global Satellite Gravity Anomaly Database V31.1, jointly maintained by David T. Sandwell (Scripps Oceanographic Institute, University of California) and Walter H. F. Smith (Satellite Altimetry Laboratory, National Oceanic and Atmospheric Administration). In the sea area, the data network size is 1'×1', the total accuracy can reach 3.03× 10−5 m/s2, and the local area can reach 1.8×10−5 m/s2. On land, the data network size is 5'×5', and the total accuracy can reach 4.125×10−5 m/s2 (Sandwell et al., 2014, 2021; Zhang et al., 2018). Because the latitude and longitude spans of the China seas and its adjacent areas are large, the influence of the Earth’s curvature cannot be ignored when conducting remote terrain correction (166.7 km). Therefore, the generalized terrain correction technique based on a fan-shaped cylinder in the spherical coordinate system was adopted to calculate the Bouguer gravity anomaly from the satellite gravity anomaly (Lei, 1984; An et al., 2010). The average density of the crust was 2.67×103 kg/m3, and the density of seawater was 1.03×103 kg/m3. As the satellite altimetry gravity anomaly in the sea area (Fig. 4a) is more accurate than that in the land area, the accuracy of the Bouguer gravity anomaly in the sea area (Fig. 4b) is still higher than that in the land area.
Magnetic data (Fig. 5a) from the World Digital Magnetic Anomaly Map 2.0 (WDMAN 2.0), co-published by the International Association of Geomagnetism and Aeronomy and the Commission for the Geological Map of the World, is the fusion result of multiple types of magnetic data from different observation forms (i.e., satellite magnetic surveys, aeromagnetic surveys, and ocean ship surveys) in different areas, and the average network size of the data is 2'×2'. Due to the wide north-south span in the China seas and its adjacent areas and the magnetic dip angle varying from −13° to 60°, the reduction to the pole of a fully variable dip angle (He et al., 2022) was adopted. By considering only induction magnetization, the reduction-to-pole magnetic anomalies in the China seas and its adjacent areas were obtained (Fig. 5b).
There are many ways to identify fractures by using gravity and magnetic anomalies. Usually, fractures are identified according to the maximum value of the total horizontal derivative of gravity and magnetic anomalies. This method has obvious advantages for large-scale fracture identification; however, it is not sensitive to small-scale fractures. To solve this problem, the NVDR-THDR is used. It can highlight weak signals and achieve better results for both larger and smaller fault identifications. Usually, the maximum position and its dislocation position in the NVDR-THDR map are used to identify the fault plane position (Wang et al., 2009; He et al., 2019; Zhu et al., 2021). In this work, we used NVDR-THDR and the fusion of gravity and magnetic anomaly (Lu et al., 2020) to identify the plane locations of faults in the China seas and its adjacent areas. The apparent depths of faults were inverted by the Tilt-Euler method based on the Bouguer gravity anomaly and the residual Bouguer gravity anomaly. The main identification mark of the plane location is the maximum line or its disconnection position of the NVDR-THDR. In the place where the maximum continuity of the NVDR-THDR is poor, it is necessary to combine the characteristics of gravity and magnetic fusion results to identify fractures. The residual Bouguer gravity anomaly is obtained by the potential field separation method based on the minimum curvature (Ji et al., 2015). The plane position of the fault is located on the inclined side of the real fault, and the apparent depth of the fault is located near the top surface of the real fault.
The Bouguer gravity anomalies in the China seas and its adjacent areas (Fig. 4b) vary from −600×10−5 m/s2 to 450×10−5 m/s2. The Bouguer gravity anomaly is primarily NE- and NNE-trending, followed by SN-trending, reflecting the stress direction of the Pacific Plate and the Philippine Plate subduction to the Eurasian Plate. The Bouguer gravity anomaly is the lowest in the northern and western continental regions and gradually rises from the continental regions to the sea. The continental Bouguer gravity anomaly shows a “low-high-low” characteristic from north to south, corresponding to the eastern Central Asian orogenic belt, the North China Plate, and the South China Plate, respectively. The Bouguer gravity anomalies in the Sea of Okhotsk, the Sea of Japan, the South China Sea Basin, the Sulu Sea, the Sulawesi Sea, and the Philippine Sea are higher than those in other regions, indicating the characteristics of ocean crust. The gravity anomaly is also found in sea basins owing to the distribution of seamounts. The trench-arc system between the China seas and the Philippine Sea presents a long and narrow low-value zone of gravity anomaly caused by the subduction of the Philippine Plate into the Eurasian Plate. The asymmetry and variation of the Bouguer gravity anomaly further indicate the asymmetry of the geological structures and the variation of crustal thickness in the China seas and its adjacent areas.
Due to the extremely complex structure of the China seas and its adjacent areas under the influence of the Eurasian Plate, the Pacific Plate, and the Indo-Australian Plate, the real magnetization direction and the adopted magnetization direction of the reduction-to-pole process are vastly different in different regions. In addition, residual magnetization also affects the direction of the dip angle. Therefore, it is impossible for reduction-to-pole magnetic anomalies to match the real magnetic anomalies of vertical magnetization because the position of the magnetic body may not exactly correspond to the position of the extreme value of the reduction-to-pole magnetic anomaly in the vertical direction. There may be some deviations, however, the reduction-to-pole magnetic anomaly is much more accurate than the total magnetic anomaly with regard to interpreting geological structures. The amplitude of the reduction-to-pole magnetic anomalies (Fig. 5b) in the China seas and its adjacent areas ranges from −650 nT to 1 300 nT, and the anomalies in the land are different from those in the sea. Similarly, the magnetic anomalies in the North China Plate have great fluctuations, and the trend is mainly NE and NW. The variation of magnetic anomalies in the South China Plate is relatively small, and the trend is mainly NE. The reduction-to-pole magnetic anomaly in the South China Sea Basin is mainly composed of many magnetic stripes. The trend of the magnetic stripes from east to west changes from EW to NE, reflecting the progressive expansion of the ocean crust from east to west. The NW-trending magnetic stripes of the Philippine Sea reflect the expansion directions of the Philippine Sea, which are NE and SW.
Based on the previous research results, ultra-crustal, and crustal faults have been identified in the China seas and its adjacent areas (Fig. 6). The strikes of the faults in the China seas and its adjacent areas are mainly NE and NW, followed by NNE, NEE, NWW, NNW, EW, and near-SN.
According to the maximum line or its disconnect position of the NVDR-THDR (Fig. 7a) of the Bouguer gravity anomaly and the NVDR-THDR (Fig. 7b) of the Moho depth (Zhang et al., 2023) in the China seas and its adjacent areas, as well as the position where anomaly characteristics of the gravity and magnetic fusion changed (Fig. 8), and combined with the previous research, a total of 58 ultra-crustal faults were inferred, most of which are block boundaries. The apparent depths of the ultra-crustal faults were obtained by the Tilt-Euler method. The plane locations and apparent depths of the ultra-crustal faults are shown in Fig. 6, and the statistical results of the fault attributes are shown in Table 1. As can be seen from Table 1, the lengths of the ultra-crustal faults are mainly between 1 000 km and 3 000 km, and the apparent depths are mainly between 10 km and 40 km. The NE trend is the main trend of the ultra-crustal faults, followed by NW, NNW, and near-SN trends.
| Fracture number | Name | Strike | Location | Properties (Tian and Luo, 2019; Yang et al., 2021) | Length/ km | Apparent depth/km | Segment number of fracture |
| F1-1 | northern margin fault of the Tuwa-Mongolia block | NW–EW–NE | northwest | compression | 1167 | 20–35 | 1 |
| F1-2 | eastern margin fault of the Tuwa-Mongolia block | NEE | northwest | compression | 1664 | 20–30 | 1 |
| F1-3 | western margin fault of the Tuwa-Mongolia block | NWW | northwest | compression | 782 | 20–35 | 1 |
| F1-4 | Altai-Erguna fault | NW–EW–NE | northwest | compression | 2986 | 20–35 | 1 |
| F1-5 | northern margin fault of North China Block | EW | northwest | compression | 3475 | 20–35 | 1 |
| F1-6 | Dabie-Qinling orogenic fault | NWW | northwest | compression | 2604 | 25–40 | 1 |
| F1-7 | Yushanjiumi fault | NWW | center | strike slip | 1273 | 20–30 | 1 |
| F1-8 | Helan-Longmenshan fault | NNE | west | compression | 2040 | 20–40 | 3 |
| F1-9 | Daxing’ anling-Taihangshan fault | NNE | northwest | strike slip | 2652 | 30–40 | 2 |
| F1-10 | Tan-Lu fault | NEE | north | strike slip | 2925 | 10–35 | 3 |
| F1-11 | Sulu orogenic fault | NEE | center | compression | 851 | 10–25 | 1 |
| F1-12 | west margin fault of the Japan Sea | NNE | northeast | subduction | 1960 | 30–40 | 1 |
| F1-13 | east margin fault of the Japan Sea | NNE | northeast | subduction | 2490 | 20–35 | 1 |
| F1-14 | western margin fault of the Okinawa Trough | NE | east | subduction | 1494 | 25–35 | 2 |
| F1-15 | eastern margin fault of the Okinawa Trough | NE | east | subduction | 2360 | 30–40 | 2 |
| F1-16 | east margin fault of Chiba Islands | NE | northeast | subduction | 1211 | 20–25 | 1 |
| F1-17 | east margin fault of Japan Island | NEE–NNE | northeast | subduction | 1631 | 20–30 | 1 |
| F1-18 | Pacific subduction fault | SN | northeast | subduction | 3502 | 25–40 | 1 |
| F1-19 | Hokkaido-Hasarin fault | NNW | northeast | subduction | 969 | 20–30 | 1 |
| F1-20 | south margin fault of the Japan Sea | NW | northeast | strike slip | 779 | 25–35 | 1 |
| F1-21 | fault of Southern Dabie Qinling orogenic belt | NWW | west | compression | 1763 | 25–35 | 1 |
| F1-22 | north Yangtze block fault | NW | center | compression | 1581 | 20–35 | 1 |
| F1-23 | south Yangtze block fault | NW | center | compression | 1324 | 25–40 | 1 |
| F1-24 | Kongkala-Lancang River combined fault | SN | west | compression | 1023 | 20–30 | 1 |
| F1-25 | Wuyishan fault | NNE | center | compression | 1561 | 20–35 | 3 |
| F1-26 | Jiangshao fault | NE | center | compression | 2453 | 20–30 | 4 |
| F1-27 | coastal fault in the northern South China Sea | NEE–NE | center | tension | 1925 | 10–35 | 4 |
| F1-28 | Red River fault | NW | west | strike slip | 2071 | 10–30 | 1 |
| F1-29 | western margin fault of Indochina block | SN | west | strike slip | 2413 | 20–30 | 2 |
| F1-30 | Mekong fault | NEE | southwest | strike slip | 1475 | 20–25 | 1 |
| F1-31 | west margin fault of South China Sea | SN | west | strike slip | 1403 | 25–35 | 1 |
| F1-32 | Xisha Trough fault | EW | center | tension | 537 | 25–35 | 1 |
| F1-33 | Mesozoic subduction fault | NE | center | subduction | 556 | 30–40 | 2 |
| F1-34 | northern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1155 | 25–35 | 1 |
| F1-35 | southern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1189 | 25–35 | 2 |
| F1-36 | Zhongnan-Liyue fault | SN | center | strike slip | 929 | 20–35 | 1 |
| F1-37 | Manila Trench fault | SN | east | subduction | 1530 | 25–35 | 3 |
| F1-38 | western margin fault of the Philippine subduction zone | SN | southeast | subduction | 1614 | 20–30 | 1 |
| F1-39 | secondary fault of Manila Trench | SN | center | subduction | 1099 | 20–35 | 2 |
| F1-40 | secondary fault of Philippine Trench | SN | southeast | subduction | 2430 | 20–30 | 1 |
| F1-41 | eastern margin fault of the Philippine subduction zone | SN | southeast | subduction | 3203 | 25–40 | 2 |
| F1-42 | western margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3596 | 20–30 | 1 |
| F1-43 | eastern margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3678 | 20–30 | 1 |
| F1-44 | Mariana Trench fault | SN | east | subduction | 3741 | 20–30 | 1 |
| F1-45 | Izu-Bonin subduction fault | NNW | east | subduction | 1914 | 10–25 | 1 |
| F1-46 | Sumatra fault | NW | southwest | compression | 1308 | 20–35 | 1 |
| F1-47 | Malacca Strait fault | NW–EW–NE | southwest | strike slip | 2330 | 10–30 | 1 |
| F1-48 | Lupal fault | NW | southwest | strike slip | 952 | 20–25 | 1 |
| F1-49 | Makassar Strait fault | NE | south | strike slip | 922 | 20–35 | 1 |
| F1-50 | Tingjia fault | NW | south | strike slip | 1397 | 20–35 | 1 |
| F1-51 | southern fault of New Guinea | NWW | southeast | subduction | 1604 | 25–35 | 1 |
| F1-52 | New Guinea subduction fault | NWW | southeast | subduction | 1666 | 25–35 | 1 |
| F1-53 | southern margin fault of the Nansha Trough | NE | south | strike slip | 997 | 20–35 | 4 |
| F1-54 | Saba-Palawan fault | NE | south | compression | 1050 | 10–30 | 4 |
| F1-55 | northern Sulu Sea fault | NE | south | tension | 618 | 25–35 | 1 |
| F1-56 | southern Sulu Sea fault | NE | south | tension | 500 | 30–40 | 1 |
| F1-57 | northern Sulawesi Sea fault | NEE | south | tension | 794 | 30–40 | 1 |
| F1-58 | southern Sulawesi Sea fault | EW | south | tension | 697 | 30–40 | 1 |
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Usually, the fracture level is divided according to its bottom interface depth. However, since the bottom interface depth of the fracture is difficult to obtain and the apparent fracture depth in this work is its top surface depth, it was difficult to determine the fracture level according to this depth. In this work, the fracture classification includes two kinds: ultra crustal faults and crustal faults. The criteria for distinguishing ultra-crustal faults from crustal faults are mainly based on the NVDR-THDR of the Moho. As shown in Fig. 7b, the faults with obvious maximum or its dislocation features in NVDR-THDR of the Moho depth are ultra-crustal faults. This is because when the bottom depth of the ultra-crustal fault cuts through the Moho, its horizontal gradient at this position is significantly changed. In addition, since NVDR-THDR of the Bouguer gravity anomaly identifies the position of the top fault surface and the NVDR-THDR of the Moho depth identifies the position near the bottom surface, the maximum value and its dislocation position of NVDR-THDR of the Moho depth are moved to the fault tendency direction.
Compared with the ultra-crustal faults, the scale of crustal faults is smaller, and due to the limited data accuracy, it is not reflected in the Bouguer gravity anomalies and the fusion results of gravity and magnetic anomalies. Therefore, the crustal faults were identified by the NVDR-THDR of the Bouguer gravity anomaly and the zero-value line of the residual Bouguer gravity anomaly (Fig. 9). A total of 140 crustal faults were inferred in the China seas and its adjacent areas. In basin regions, faults mainly control the formation and evolution of basins. The apparent depth of crustal faults is obtained by the Tilt-Euler method using the residual Bouguer gravity anomaly. The plane locations and apparent depths of the crustal faults are shown in Fig. 6, it shows that the lengths of crustal faults are mainly between 300 km and 1 000 km, and the apparent depths are mainly in the range of 0–20 km. The crustal faults are mainly NE- and NW-trending, followed by EW-, and SN-trending.
Dozens of sedimentary basins exist in the China seas and nearby areas (Fig. 1), most of which are distributed in continental areas and margins. According to the differences in basin structure and genesis, basins can be divided into seven types (Table 2) (Chen et al., 2019). The results of the oil and gas resource dynamic evaluation of China in 2015 showed that the geological resources of oil in 11 offshore Cenozoic basins (Bohai Bay, North Yellow Sea, South Yellow Sea, East China Sea, Okinawa Trough, Taixi, Taixinan, Zhujiang River (Pearl River) Estuary, Beibu Gulf, Qiongdongnan, and Yinggehai) are 239.04×108 t, and the resources in the Bohai Bay, Zhujiang River Estuary, Beibu Gulf, and Qiongdongnan are over 10×108 t, accumulatively 220.67×108 t, accounting for 92% of the total resources. The geological resources of natural gas are 20.85×1012 m3, the resources of the five major basins, the East China Sea, Qiongdongnan, Yinggehai, Zhujiang River Estuary, and Bohai Bay, exceed 1012 m3, accumulatively 19.92×1012 m3, accounting for 96% of the total resources. In addition, the sea near the Xisha and Nansha Islands in the South China Sea has an area of 82×104 km2 and involves rich oil and gas resources. To sum up, the basins have a very broad prospect for oil and gas exploration in the China seas and its adjacent areas. Moreover, faults are closely related to the mineralization and accumulation of oil and gas, controlling the formation and evolution of the basin. Therefore, it is of great significance to study the control of faults on petroliferous basins to predict the mineralization and accumulation of oil and gas reservoirs.
| Type of basin | Name of basin |
| Intracontinental rift basin | Hailar Basin, Erlian Basin, Ordos Basin, Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin, Sanjiang Basin, North Yellow Sea Basin, Subei Basin, South Yellow Sea Basin, Beibu Gulf Basin |
| Continental margin rift basin | East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Pearl River Estuary Basin, Qiongdongnan Basin |
| Strike-slip pull-apart basin | Chuxiong Basin, Lanping-Simao Basin, Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nabweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin |
| Back-arc basin | Okinawa Trough Basin |
| Fore-arc basin | Brunei-Sabah Basin |
| Foreland basin | Zengmu Basin |
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According to the identified faults, the main ultra-crustal faults controlling the basins in the China seas and its adjacent areas include the following: the northern margin fault of North China Block, Dabie-Qinling orogenic fault, Yushanjiumi fault, Red River fault, the western margin fault of the South China Sea, Jiangshao fault, the coastal fault in the northern South China Sea, Mesozoic subduction fault, Xisha Trough fault, Lupar fault, Brunei-Sabah fault, the Helan-Longmenshan fault, Daxing’anling-Taihangshan fault, Wuyishan fault, Tan-Lu fault, Sulu orogenic fault, Tingjia fault, and the southern margin fault of the Nansha Trough. Based on faults and their apparent depths, gravity and magnetic fusion results, and the distribution and properties of basins, the types of petroliferous basins in the China seas and its adjacent areas were further refined (Fig. 10, Table 3). The main differences between the classification results and previous research results can be summarized as follows: the intracontinental rift basins are divided into three areas from east to west (the first area includes the Hailaer, Erlian, Ordos, Sichuan, Chuxiong, and Lanping-Simao basins, the second area includes the Songliao, Bohai Bay, South North China, Nanxiang, Jianghan, and Beibu Gulf basins, and the third area includes the Sanjiang, North Yellow Sea, Subei, and South Yellow Sea basins). The East China Sea Shelf Basin in the continental margin rift basins is divided into north and south, and the north is a separate sector. The reason for this difference between the results of this basin type division and the previous results is that the previous basin types were divided according to the formation and evolution process of the basin, however, this time, the basin types are classified according to faults, gravity and magnetic anomalies, and the previous results. For the relationship between the faults and oil and gas basins, the main influencing factors are the distance between the faults and the oil and gas fields in the basin, the depth of the faults (top surface depth and bottom interface depth), and the fault property (strike-slip, tension, compression, etc.), the thickness of sedimentary layer near the fracture. These influencing factors for oil and gas basins are very complex. At present, the discovered oil and gas fields are generally located on the sides of the deep-large faults or the intersections of two faults, where the thickness of the sedimentary layer is larger. Therefore, the locations close to deep faults and with a large thickness of the sedimentary layer are favorable positions for oil and gas development. The data of sedimentary layer thickness in this work are from Crust1.0-A1-degree global model(Laske et al., 2013) and joint inversion results of gravity and seismic data(Feng et al., 2018). Regarding the apparent depth of the fracture, since the fracture is a migration channel of oil and gas, when the apparent depth is less than the depth of the bottom interface of the sedimentary layer, it is beneficial to the migration of oil and gas. Based on the above-mentioned relationship, we attempted to consider the distance between the faults and the oil and gas fields in the basin, the thickness of the sedimentary layer and the apparent depth of the fault (top surface depth) to put forward the concept of the influencing factor of faults for the first time. The calculation formula of this factor is as follows:
| $$ {f_i} = \frac{{\displaystyle\sum\limits_{{l_{i,j}} < R} {\frac{{{h_i}}}{{({l_{i,j}} + \alpha ){d_{i,j}}}}} }}{{\max \left\{ {{\left(\displaystyle\sum\limits_{{l_{i,j}} < R} {\frac{{{h_i}}}{{({l_{i,j}} + \alpha ){d_{i,j}}}}} \right)}_i}\right\} }} , $$ | (1) |
where i is the serial number of the observation points, R is the radius centered at the i-th point, j is the serial number of the fault points within the radius R,
| Type of basin | Name of basin | Faults controlling the basins | |
| Previous study | This study | ||
| Intracontinental rift basin | First region | Hailaer Basin, Erlian Basin, Ordos Basin and Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Helan-Longmenshan fault, Daxing’an ling-Taihangshan fault, Wuyishan fault |
| Second region | Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin and Beibu Gulf Basin | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Daxing’anling-Taihangshan fault, Wuyishan fault, Tan-Lu fault | |
| Third region | Sanjiang Basin, North Yellow Sea Basin, Subei Basin and South Yellow Sea Basin | he northern margin fault of the North China Block, Yushanjiumi fault, Tan-Lu fault, Sulu orogenic fault | |
| Continental margin rift basin | First region | north part of the East China Sea Shelf Basin | Jiangshao fault, Yushanjiumi fault |
| Second region | south part of the East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Zhujiang River Estuary Basin, Qiongdongnan Basin | Yushanjiumi fault, The coastal fault in the northern South China Sea, Mesozoic subduction fault, Xisha Trough fault | |
| Strike-slip pull-apart basin | Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin | Red River fault, West margin fault of South China Sea | |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nanweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin | southern boundary of the oceanic crust in the South China Sea, the southern margin fault of the Nansha Trough, western margin fault of the South China Sea, the Tingjia fault | |
| Back-arc basin | First region | north part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough |
| Second region | south part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough | |
| Fore-arc basin | Brunei-Sabah Basin | southern margin fault of Nansha Trough, Sabah-Palawan fault | |
| Foreland basin | Zengmu Basin | Lupal fault, Tingjia fault | |
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The influence factor of the faults (Fig. 11 ) shows that the oil and gas fields that have been discovered are basically distributed at its high values. Therefore, the key areas for oil and gas exploration were predicted, as described in detail below.
(1) Intracontinental rift basins
Intracontinental rift basins include the Hailar, Erlian, Ordos, Sichuan, Chuxiong, Lanping-Simao, Songliao, Bohai Bay, south North China, Nanxiang, Jianghan, Sanjiang, North Yellow Sea, Subei, South Yellow Sea, and Beibu Gulf basins. The fracture distribution feature showed that the intracontinental rift basins can be divided into three areas (from west to east). The first area involves the Hailar, Erlian, Ordos, Sichuan, Chuxiong, and Lanping-Simao basins; the second area involves the Songliao, Bohai Bay, South North China, Nanxiang, Jianghan, and Beibu Gulf basins; and the third area involves the Sanjiang, North Yellow Sea, South Yellow Sea, and Subei basins. From the distribution of the oil and gas fields collected, we inferred that the oil and gas fields in the first area are distributed in the center of the basin and controlled by crustal faults; the oil and gas fields of the Songliao Basin in the second area are also distributed in the center of the basin, but the oil and gas fields in Bohai Bay Basin are distributed on the side of the Tan-Lu fault. It is due to the influence of the dextral strike-slip tension-torsion or compression-torsion action of the NE-trending Tan-Lu fault, which forms large traps in the depression, dip, or steep slope of the fault. These traps are usually double depressions for hydrocarbon supply or close to hydrocarbon generation centers (Lv, 2012) and are long-term direction zones for hydrocarbon migration and accumulation. Therefore, the Bohai Bay Basin is extraordinarily rich in oil and gas. There are no proven oil and gas fields in the third area. In conclusion, the Tan-Lu fault plays a positive role in the generation and migration of oil and gas. It can also be seen from Fig. 11 that the oil and gas fields in the Bohai Bay Basin are mostly distributed at the high value areas of the influence factor. Therefore, high value area of influence factor in the east of South North China Basin is predicted to be the key area of oil and gas exploration.
(2) Continental margin rift basins
Continental margin rift basins include the East China Sea Shelf Basin, Taixi, Taixinan, Zhujiang River Estuary, and Qiongdongnan basins. The basins are controlled by the Jiangshao fault, the Yushanjiumi fault, the coastal fault in the northern South China Sea, the Mesozoic subduction fault, and the Xisha Trough fault, which are NEE trending, located in the active continental margin and belong to the continental margin basin. From the apparent depth inversion results (Fig. 6), the Yushanjiumi fault extends to the land in the northwest direction and gets connected with the Qinling-Dabie orogenic belt, which divides the East China Sea Shelf Basin into two parts: the north part and the south part. The inversion results also show that the depth of the north part is shallower than that of the south part. In addition, the gravity and magnetic anomaly fusion results show that the anomaly characteristics in the north part are similar from east to west. Therefore, the East China Sea Shelf Basin in the continental margin rift basin is divided into two regions. The north belongs to the first region, controlled by the Jiangshao fault, striking NE. The south of the East China Sea Shelf Basin and the Taixi, Taixinan, Zhujiang River Estuary, and Qiongdongnan basins belong to the second region, which is distributed along the coastal fault in the northern South China Sea. It can be seen from the discovered oil and gas distribution map that the Zhujiang River Estuary and the Beibu Gulf basins are rich in oil and gas. In particular, the Zhujiang River Estuary Basin has accumulated more than 10×108 t proven oil reserves and 1 800×108 m3 proven natural gas reserves. In addition, some oil and gas fields are distributed on both sides of the Yushanjiumi fault in the East China Sea Shelf Basin. As a result, the coastal fault in the northern South China Sea and the Yushanjiumi fault play a positive role in hydrocarbon generation and migration. Figure 11 also shows that the oil and gas fields in the Zhujiang River Estuary Basin and East China Sea Shelf Basin are distributed at the high value areas of the influence factor. Therefore, the southeast region of East China Sea Shelf Basin, the Taixinan, and Qiongdongnan basins are the key areas for oil and gas exploration.
(3) Strike-slip pull-apart basins
The strike-slip pull-apart basin area is controlled by the Red River fault and the western margin fault of the South China Sea. The overall strike of the basin area is near NW−SN, including the Yinggehai, Zhongjiannan, and Wan’an basins. The Red River fault and the western margin fault of the South China Sea are strike-slip faults. Harding (1973) studied the strike-slip traps and found that oil and gas in the strike-slip pull-apart basin were mainly distributed along the strike-slip belt, and the echelon structure formed by the strike-slip activity could serve as an oil accumulation trap. The high heat flow caused by large-boundary strike-slip faults communicating with deep rock mass is conducive to the evolution of source rocks in pull-apart basins (Lees, 2002; Cunningham and Mann, 2007). Strike-slip transformation structure can be used as a favorable channel to connect sand bodies and oil sources (Martel, 1990; Wang et al., 2011). It is also a favorable zone for oil and gas migration and accumulation (Zhu et al., 2009a), which can be proved from the oil and gas distribution map. Therefore, besides the Yinggehai and Wan’an basins, it can be seen from Fig. 11 that the Zhongjiannan Basin should also be considered a key area for oil and gas exploration in the strike-slip pull-apart basins. In addition, the Nanweixi Basin located in the east of the western margin fault of the South China Sea is a key area for oil and gas exploration.
(4) Rifted continental basins
The rifted continental basins are bounded by the southern boundary of the oceanic crust in the north, the southern margin fault of the Nansha Trough in the south, and the Tingjia fault and the western margin fault of the South China Sea in the west. The basins are NE-trending, including the Beikang, Nanweixi, Nanweidong, Andubei, Yongshu, Jiuzhang, and Liyue basins. Due to plate compression and collision, the structure of the area is complex, and the degree of oil and gas exploration is low. However, it can be seen from the oil and gas distribution map that in the south of the southern margin fault of the Nansha Trough, the North Palawan and the Brunei-Sabah basins are rich in oil and gas, which shows that this fault positively influences oil and gas generation and migration. Figure 11 shows that the Liyue Basin is also located in the high value areas of the influence factor. Therefore, this region could be considered as a focus area for oil and gas exploration.
(5) Backarc basins
The Okinawa Trough Basin is a backarc basin divided into northern and southern parts by the Yushanjiumi fault, which is similar to the East China Sea Shelf Basin. Similarly, the inversion results of the apparent depths of faults indicate significant differences between the characteristics of the northern and southern parts. The apparent depths of the northern faults with NE trend influenced by the Jiangshao fault are shallower than that of the southern faults with NEE trend influenced by the coastal fault in the northern South China Sea. Figure 11 also shows that the central region of Okinawa Trough Basin at high value areas could be the focus areas for oil and gas exploration.
(6) Forearc basins
The NE-trending Brunei-Sabah Basin belongs to the forearc basin, which is controlled by the southern margin fault of the Nansha Trough and the Sabah-Palawan fault. The results show that the basin is rich in oil and gas resources.
(7) Foreland basins
The Zengmu Basin is a foreland basin, bounded by the Tingjia fault in the north and the Lupal fault in the south. The overall trend of the basin is nearly EW. Affected by the two faults, the Zengmu Basin is a typical oil-gas-rich basin with 50.79×108 t of proven oil and gas reserves. Thus, the Tingjia fault positively affects oil and gas generation and migration, and the Beikang Basin on the east side of the fault is another key area for oil and gas exploration. The high value areas in Fig. 11 also support this region as a key exploration area.
In conclusion, the first and second regions of intracontinental rift basins are controlled by the northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Helan-Longmenshan fault, Daxing’an ling-Taihangshan fault, Wuyishan fault, and Tan-Lu fault, which are rich in oil and gas. Among these faults, the Tan-Lu fault plays a positive role in the formation and migration of oil and gas. The east of South North China Basin can be used as a key area for oil and gas exploration. The third region is controlled by the Yushanjiumi fault and the Sulu orogenic fault, which is lean oil and gas areas. The continental margin rift basins are mainly controlled by the coastal fault in the northern South China Sea and the Yushanjiumi fault. The first zone is poor in oil and gas, while the second zone is rich in oil and gas. In this area, the southeast region of East China Sea Shelf Basin, the Taixinan, and Qiongdongnan basins are the key areas for oil and gas exploration. Strike-slip pull-apart basins are controlled by the Red River fault and the western margin fault of the South China Sea. Besides the Yinggehai and Wan’an basins, the Zhongjiannan Basin should also be considered a key area for oil and gas exploration. The rifted continental basins are controlled by the western margin fault of the South China Sea, the southern margin fault of the Nansha Trough, and the Tingjia fault, and the exploration degree is relatively low. However, affected by the three faults, the Liyue, Beikang, and Nanweixi basins can be regarded as key areas for oil and gas exploration.
Based on the analysis of the gravity and magnetic data as well as the existing geological data in the China seas and its adjacent areas, the following conclusions can be drawn:
(1) A total of 198 faults were identified in the China seas and its adjacent areas: 58 ultra-crustal faults, and 140 crustal faults. The faults are mainly NE- and NW-trending, followed by EW-, and nearly SN-trending. The ultra-crustal faults are 1 000–3 000 km in length and 10–40 km in apparent depth; the crustal faults are 300–1 000 km in length and 0–20 km in apparent depth.
(2) The types of oil- and gas-rich basins were further refined based on the plane positions and apparent depths of faults in the China seas and its adjacent areas, and the influence factor of faults is put forward to predict the key areas for oil and gas exploration. The intracontinental rift basin can be divided into three zones from west to east, and the east of South North China Basin is considered a key area for oil and gas exploration. In the continental margin rift basins, the southeast region of East China Sea Shelf Basin, the Taixinan and Qiongdongnan basins can be used as the key areas for oil and gas exploration. Strike-slip pull-apart basins are controlled by the Red River fault and the western margin fault of the South China Sea; besides the Yinggehai and the Wan’an basins, the Zhongjiannan Basin is considered a key area for oil and gas exploration. Affected by the western margin fault of the South China Sea, the southern Nansha Trough fault and the Tingjia fault, the Liyue, the Beikang, and the Nanweixi basins in the rifted continental basins can be regarded as key areas for oil and gas exploration.
Through this study, we obtained a basic understanding of the plane distributions and depth characteristics of the faults in the China seas and its adjacent areas, as well as the basin subdivisions. However, an in-depth fault depth study will be conducted using geophysical (gravity, magnetic, and seismic) data.
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Figures(11) / Tables(3)
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Xin’gang Luo, Wanyin Wang, Ying Chen, Zhizhao Bai, Dingding Wang, Tao He, Yimi Zhang, Ruiyun Ma. Study on the distribution characteristics of faults and their control over petroliferous basins in the China seas and its adjacent areas[J]. Acta Oceanologica Sinica, 2023, 42(3): 227-242. doi: 10.1007/s13131-022-2138-6
| Fracture number | Name | Strike | Location | Properties (Tian and Luo, 2019; Yang et al., 2021) | Length/ km | Apparent depth/km | Segment number of fracture |
| F1-1 | northern margin fault of the Tuwa-Mongolia block | NW–EW–NE | northwest | compression | 1167 | 20–35 | 1 |
| F1-2 | eastern margin fault of the Tuwa-Mongolia block | NEE | northwest | compression | 1664 | 20–30 | 1 |
| F1-3 | western margin fault of the Tuwa-Mongolia block | NWW | northwest | compression | 782 | 20–35 | 1 |
| F1-4 | Altai-Erguna fault | NW–EW–NE | northwest | compression | 2986 | 20–35 | 1 |
| F1-5 | northern margin fault of North China Block | EW | northwest | compression | 3475 | 20–35 | 1 |
| F1-6 | Dabie-Qinling orogenic fault | NWW | northwest | compression | 2604 | 25–40 | 1 |
| F1-7 | Yushanjiumi fault | NWW | center | strike slip | 1273 | 20–30 | 1 |
| F1-8 | Helan-Longmenshan fault | NNE | west | compression | 2040 | 20–40 | 3 |
| F1-9 | Daxing’ anling-Taihangshan fault | NNE | northwest | strike slip | 2652 | 30–40 | 2 |
| F1-10 | Tan-Lu fault | NEE | north | strike slip | 2925 | 10–35 | 3 |
| F1-11 | Sulu orogenic fault | NEE | center | compression | 851 | 10–25 | 1 |
| F1-12 | west margin fault of the Japan Sea | NNE | northeast | subduction | 1960 | 30–40 | 1 |
| F1-13 | east margin fault of the Japan Sea | NNE | northeast | subduction | 2490 | 20–35 | 1 |
| F1-14 | western margin fault of the Okinawa Trough | NE | east | subduction | 1494 | 25–35 | 2 |
| F1-15 | eastern margin fault of the Okinawa Trough | NE | east | subduction | 2360 | 30–40 | 2 |
| F1-16 | east margin fault of Chiba Islands | NE | northeast | subduction | 1211 | 20–25 | 1 |
| F1-17 | east margin fault of Japan Island | NEE–NNE | northeast | subduction | 1631 | 20–30 | 1 |
| F1-18 | Pacific subduction fault | SN | northeast | subduction | 3502 | 25–40 | 1 |
| F1-19 | Hokkaido-Hasarin fault | NNW | northeast | subduction | 969 | 20–30 | 1 |
| F1-20 | south margin fault of the Japan Sea | NW | northeast | strike slip | 779 | 25–35 | 1 |
| F1-21 | fault of Southern Dabie Qinling orogenic belt | NWW | west | compression | 1763 | 25–35 | 1 |
| F1-22 | north Yangtze block fault | NW | center | compression | 1581 | 20–35 | 1 |
| F1-23 | south Yangtze block fault | NW | center | compression | 1324 | 25–40 | 1 |
| F1-24 | Kongkala-Lancang River combined fault | SN | west | compression | 1023 | 20–30 | 1 |
| F1-25 | Wuyishan fault | NNE | center | compression | 1561 | 20–35 | 3 |
| F1-26 | Jiangshao fault | NE | center | compression | 2453 | 20–30 | 4 |
| F1-27 | coastal fault in the northern South China Sea | NEE–NE | center | tension | 1925 | 10–35 | 4 |
| F1-28 | Red River fault | NW | west | strike slip | 2071 | 10–30 | 1 |
| F1-29 | western margin fault of Indochina block | SN | west | strike slip | 2413 | 20–30 | 2 |
| F1-30 | Mekong fault | NEE | southwest | strike slip | 1475 | 20–25 | 1 |
| F1-31 | west margin fault of South China Sea | SN | west | strike slip | 1403 | 25–35 | 1 |
| F1-32 | Xisha Trough fault | EW | center | tension | 537 | 25–35 | 1 |
| F1-33 | Mesozoic subduction fault | NE | center | subduction | 556 | 30–40 | 2 |
| F1-34 | northern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1155 | 25–35 | 1 |
| F1-35 | southern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1189 | 25–35 | 2 |
| F1-36 | Zhongnan-Liyue fault | SN | center | strike slip | 929 | 20–35 | 1 |
| F1-37 | Manila Trench fault | SN | east | subduction | 1530 | 25–35 | 3 |
| F1-38 | western margin fault of the Philippine subduction zone | SN | southeast | subduction | 1614 | 20–30 | 1 |
| F1-39 | secondary fault of Manila Trench | SN | center | subduction | 1099 | 20–35 | 2 |
| F1-40 | secondary fault of Philippine Trench | SN | southeast | subduction | 2430 | 20–30 | 1 |
| F1-41 | eastern margin fault of the Philippine subduction zone | SN | southeast | subduction | 3203 | 25–40 | 2 |
| F1-42 | western margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3596 | 20–30 | 1 |
| F1-43 | eastern margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3678 | 20–30 | 1 |
| F1-44 | Mariana Trench fault | SN | east | subduction | 3741 | 20–30 | 1 |
| F1-45 | Izu-Bonin subduction fault | NNW | east | subduction | 1914 | 10–25 | 1 |
| F1-46 | Sumatra fault | NW | southwest | compression | 1308 | 20–35 | 1 |
| F1-47 | Malacca Strait fault | NW–EW–NE | southwest | strike slip | 2330 | 10–30 | 1 |
| F1-48 | Lupal fault | NW | southwest | strike slip | 952 | 20–25 | 1 |
| F1-49 | Makassar Strait fault | NE | south | strike slip | 922 | 20–35 | 1 |
| F1-50 | Tingjia fault | NW | south | strike slip | 1397 | 20–35 | 1 |
| F1-51 | southern fault of New Guinea | NWW | southeast | subduction | 1604 | 25–35 | 1 |
| F1-52 | New Guinea subduction fault | NWW | southeast | subduction | 1666 | 25–35 | 1 |
| F1-53 | southern margin fault of the Nansha Trough | NE | south | strike slip | 997 | 20–35 | 4 |
| F1-54 | Saba-Palawan fault | NE | south | compression | 1050 | 10–30 | 4 |
| F1-55 | northern Sulu Sea fault | NE | south | tension | 618 | 25–35 | 1 |
| F1-56 | southern Sulu Sea fault | NE | south | tension | 500 | 30–40 | 1 |
| F1-57 | northern Sulawesi Sea fault | NEE | south | tension | 794 | 30–40 | 1 |
| F1-58 | southern Sulawesi Sea fault | EW | south | tension | 697 | 30–40 | 1 |
DownLoad:
CSV
| Type of basin | Name of basin |
| Intracontinental rift basin | Hailar Basin, Erlian Basin, Ordos Basin, Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin, Sanjiang Basin, North Yellow Sea Basin, Subei Basin, South Yellow Sea Basin, Beibu Gulf Basin |
| Continental margin rift basin | East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Pearl River Estuary Basin, Qiongdongnan Basin |
| Strike-slip pull-apart basin | Chuxiong Basin, Lanping-Simao Basin, Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nabweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin |
| Back-arc basin | Okinawa Trough Basin |
| Fore-arc basin | Brunei-Sabah Basin |
| Foreland basin | Zengmu Basin |
DownLoad:
CSV
| Type of basin | Name of basin | Faults controlling the basins | |
| Previous study | This study | ||
| Intracontinental rift basin | First region | Hailaer Basin, Erlian Basin, Ordos Basin and Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Helan-Longmenshan fault, Daxing’an ling-Taihangshan fault, Wuyishan fault |
| Second region | Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin and Beibu Gulf Basin | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Daxing’anling-Taihangshan fault, Wuyishan fault, Tan-Lu fault | |
| Third region | Sanjiang Basin, North Yellow Sea Basin, Subei Basin and South Yellow Sea Basin | he northern margin fault of the North China Block, Yushanjiumi fault, Tan-Lu fault, Sulu orogenic fault | |
| Continental margin rift basin | First region | north part of the East China Sea Shelf Basin | Jiangshao fault, Yushanjiumi fault |
| Second region | south part of the East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Zhujiang River Estuary Basin, Qiongdongnan Basin | Yushanjiumi fault, The coastal fault in the northern South China Sea, Mesozoic subduction fault, Xisha Trough fault | |
| Strike-slip pull-apart basin | Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin | Red River fault, West margin fault of South China Sea | |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nanweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin | southern boundary of the oceanic crust in the South China Sea, the southern margin fault of the Nansha Trough, western margin fault of the South China Sea, the Tingjia fault | |
| Back-arc basin | First region | north part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough |
| Second region | south part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough | |
| Fore-arc basin | Brunei-Sabah Basin | southern margin fault of Nansha Trough, Sabah-Palawan fault | |
| Foreland basin | Zengmu Basin | Lupal fault, Tingjia fault | |
DownLoad:
CSV
| Fracture number | Name | Strike | Location | Properties (Tian and Luo, 2019; Yang et al., 2021) | Length/ km | Apparent depth/km | Segment number of fracture |
| F1-1 | northern margin fault of the Tuwa-Mongolia block | NW–EW–NE | northwest | compression | 1167 | 20–35 | 1 |
| F1-2 | eastern margin fault of the Tuwa-Mongolia block | NEE | northwest | compression | 1664 | 20–30 | 1 |
| F1-3 | western margin fault of the Tuwa-Mongolia block | NWW | northwest | compression | 782 | 20–35 | 1 |
| F1-4 | Altai-Erguna fault | NW–EW–NE | northwest | compression | 2986 | 20–35 | 1 |
| F1-5 | northern margin fault of North China Block | EW | northwest | compression | 3475 | 20–35 | 1 |
| F1-6 | Dabie-Qinling orogenic fault | NWW | northwest | compression | 2604 | 25–40 | 1 |
| F1-7 | Yushanjiumi fault | NWW | center | strike slip | 1273 | 20–30 | 1 |
| F1-8 | Helan-Longmenshan fault | NNE | west | compression | 2040 | 20–40 | 3 |
| F1-9 | Daxing’ anling-Taihangshan fault | NNE | northwest | strike slip | 2652 | 30–40 | 2 |
| F1-10 | Tan-Lu fault | NEE | north | strike slip | 2925 | 10–35 | 3 |
| F1-11 | Sulu orogenic fault | NEE | center | compression | 851 | 10–25 | 1 |
| F1-12 | west margin fault of the Japan Sea | NNE | northeast | subduction | 1960 | 30–40 | 1 |
| F1-13 | east margin fault of the Japan Sea | NNE | northeast | subduction | 2490 | 20–35 | 1 |
| F1-14 | western margin fault of the Okinawa Trough | NE | east | subduction | 1494 | 25–35 | 2 |
| F1-15 | eastern margin fault of the Okinawa Trough | NE | east | subduction | 2360 | 30–40 | 2 |
| F1-16 | east margin fault of Chiba Islands | NE | northeast | subduction | 1211 | 20–25 | 1 |
| F1-17 | east margin fault of Japan Island | NEE–NNE | northeast | subduction | 1631 | 20–30 | 1 |
| F1-18 | Pacific subduction fault | SN | northeast | subduction | 3502 | 25–40 | 1 |
| F1-19 | Hokkaido-Hasarin fault | NNW | northeast | subduction | 969 | 20–30 | 1 |
| F1-20 | south margin fault of the Japan Sea | NW | northeast | strike slip | 779 | 25–35 | 1 |
| F1-21 | fault of Southern Dabie Qinling orogenic belt | NWW | west | compression | 1763 | 25–35 | 1 |
| F1-22 | north Yangtze block fault | NW | center | compression | 1581 | 20–35 | 1 |
| F1-23 | south Yangtze block fault | NW | center | compression | 1324 | 25–40 | 1 |
| F1-24 | Kongkala-Lancang River combined fault | SN | west | compression | 1023 | 20–30 | 1 |
| F1-25 | Wuyishan fault | NNE | center | compression | 1561 | 20–35 | 3 |
| F1-26 | Jiangshao fault | NE | center | compression | 2453 | 20–30 | 4 |
| F1-27 | coastal fault in the northern South China Sea | NEE–NE | center | tension | 1925 | 10–35 | 4 |
| F1-28 | Red River fault | NW | west | strike slip | 2071 | 10–30 | 1 |
| F1-29 | western margin fault of Indochina block | SN | west | strike slip | 2413 | 20–30 | 2 |
| F1-30 | Mekong fault | NEE | southwest | strike slip | 1475 | 20–25 | 1 |
| F1-31 | west margin fault of South China Sea | SN | west | strike slip | 1403 | 25–35 | 1 |
| F1-32 | Xisha Trough fault | EW | center | tension | 537 | 25–35 | 1 |
| F1-33 | Mesozoic subduction fault | NE | center | subduction | 556 | 30–40 | 2 |
| F1-34 | northern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1155 | 25–35 | 1 |
| F1-35 | southern boundary of the oceanic crust in the South China Sea | NE | central south | tension | 1189 | 25–35 | 2 |
| F1-36 | Zhongnan-Liyue fault | SN | center | strike slip | 929 | 20–35 | 1 |
| F1-37 | Manila Trench fault | SN | east | subduction | 1530 | 25–35 | 3 |
| F1-38 | western margin fault of the Philippine subduction zone | SN | southeast | subduction | 1614 | 20–30 | 1 |
| F1-39 | secondary fault of Manila Trench | SN | center | subduction | 1099 | 20–35 | 2 |
| F1-40 | secondary fault of Philippine Trench | SN | southeast | subduction | 2430 | 20–30 | 1 |
| F1-41 | eastern margin fault of the Philippine subduction zone | SN | southeast | subduction | 3203 | 25–40 | 2 |
| F1-42 | western margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3596 | 20–30 | 1 |
| F1-43 | eastern margin fault of Palau Ridge in Kyushu | SN | southeast | tension | 3678 | 20–30 | 1 |
| F1-44 | Mariana Trench fault | SN | east | subduction | 3741 | 20–30 | 1 |
| F1-45 | Izu-Bonin subduction fault | NNW | east | subduction | 1914 | 10–25 | 1 |
| F1-46 | Sumatra fault | NW | southwest | compression | 1308 | 20–35 | 1 |
| F1-47 | Malacca Strait fault | NW–EW–NE | southwest | strike slip | 2330 | 10–30 | 1 |
| F1-48 | Lupal fault | NW | southwest | strike slip | 952 | 20–25 | 1 |
| F1-49 | Makassar Strait fault | NE | south | strike slip | 922 | 20–35 | 1 |
| F1-50 | Tingjia fault | NW | south | strike slip | 1397 | 20–35 | 1 |
| F1-51 | southern fault of New Guinea | NWW | southeast | subduction | 1604 | 25–35 | 1 |
| F1-52 | New Guinea subduction fault | NWW | southeast | subduction | 1666 | 25–35 | 1 |
| F1-53 | southern margin fault of the Nansha Trough | NE | south | strike slip | 997 | 20–35 | 4 |
| F1-54 | Saba-Palawan fault | NE | south | compression | 1050 | 10–30 | 4 |
| F1-55 | northern Sulu Sea fault | NE | south | tension | 618 | 25–35 | 1 |
| F1-56 | southern Sulu Sea fault | NE | south | tension | 500 | 30–40 | 1 |
| F1-57 | northern Sulawesi Sea fault | NEE | south | tension | 794 | 30–40 | 1 |
| F1-58 | southern Sulawesi Sea fault | EW | south | tension | 697 | 30–40 | 1 |
| Type of basin | Name of basin |
| Intracontinental rift basin | Hailar Basin, Erlian Basin, Ordos Basin, Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin, Sanjiang Basin, North Yellow Sea Basin, Subei Basin, South Yellow Sea Basin, Beibu Gulf Basin |
| Continental margin rift basin | East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Pearl River Estuary Basin, Qiongdongnan Basin |
| Strike-slip pull-apart basin | Chuxiong Basin, Lanping-Simao Basin, Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nabweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin |
| Back-arc basin | Okinawa Trough Basin |
| Fore-arc basin | Brunei-Sabah Basin |
| Foreland basin | Zengmu Basin |
| Type of basin | Name of basin | Faults controlling the basins | |
| Previous study | This study | ||
| Intracontinental rift basin | First region | Hailaer Basin, Erlian Basin, Ordos Basin and Sichuan Basin, Chuxiong Basin and Lanping-Simao Basin, | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Helan-Longmenshan fault, Daxing’an ling-Taihangshan fault, Wuyishan fault |
| Second region | Songliao Basin, Bohai Bay Basin, South North China Basin, Nanxiang Basin, Jianghan Basin and Beibu Gulf Basin | northern margin fault of the North China Block, Dabie-Qinling orogenic fault, Daxing’anling-Taihangshan fault, Wuyishan fault, Tan-Lu fault | |
| Third region | Sanjiang Basin, North Yellow Sea Basin, Subei Basin and South Yellow Sea Basin | he northern margin fault of the North China Block, Yushanjiumi fault, Tan-Lu fault, Sulu orogenic fault | |
| Continental margin rift basin | First region | north part of the East China Sea Shelf Basin | Jiangshao fault, Yushanjiumi fault |
| Second region | south part of the East China Sea Shelf Basin, Taixi Basin, Taixinan Basin, Zhujiang River Estuary Basin, Qiongdongnan Basin | Yushanjiumi fault, The coastal fault in the northern South China Sea, Mesozoic subduction fault, Xisha Trough fault | |
| Strike-slip pull-apart basin | Yinggehai Basin, Zhongjiannan Basin, Wan’an Basin | Red River fault, West margin fault of South China Sea | |
| Rifted continental basin | Beikang Basin, Liyue Basin, Nanweixi Basin, Nanweidong Basin, Yongshu Basin, Jiuzhang Basin, Andubei Basin, North Palawan Basin, South Palawan Basin | southern boundary of the oceanic crust in the South China Sea, the southern margin fault of the Nansha Trough, western margin fault of the South China Sea, the Tingjia fault | |
| Back-arc basin | First region | north part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough |
| Second region | south part of Okinawa Trough Basin | Yushanjiumi fault, western margin fault of Okinawa trough, eastern margin fault of Okinawa trough | |
| Fore-arc basin | Brunei-Sabah Basin | southern margin fault of Nansha Trough, Sabah-Palawan fault | |
| Foreland basin | Zengmu Basin | Lupal fault, Tingjia fault | |
DownLoad:
DownLoad:
