Abstract
WNW-directed faults are widespread in eastern China, but debates regarding their distributions and evolutionary processes remain unsettled. Based on the latest 3-D seismic data, a series of WNW-directed faults south of the Liaodong Bay subbasin was identified, for which the evolution and formation mechanisms were discussed. The results show that four WNW-directed faults are characterized by poor continuity and nearly parallel orientations. Vertically, they exhibit listric geometries and cut through Paleozoic and Mesozoic formations. Since the late Triassic, these faults began as reverse faults under nearly S-N horizontal compression. In the Jurassic, those faults maintained their reverse-faulting activities with dramatically decreased intensities. In the Early Cretaceous, the WNW-directed faults were changed into normal faults under regional extension and were influenced by the sinistral strike-slip movement along the Tan-Lu fault zone. In the Late Cretaceous, the WNW-directed normal faults probably stopped moving due to a regional compressional event. During the Paleogene, the WNW-directed faults were reactivated with decreased intensities and were cut by NNE-directed faults. Here, we emphasize that the evolution of the WNW-directed faults could shed light on the regional tectonics. The WNW-trending faults that developed in the Liaodong Bay subbasin are closely related to the faults in the Yanshan orogenic belt. Therefore, investigating the characteristics and origin of WNW-induced faults will provide evidence for the tectonic evolution of the North China Block. In addition, the development of WNW-directed faults in the southern Liaodong Bay subbasin was conducive to the formation of buried Mesozoic and Paleozoic hills and hydrocarbon accumulations. In addition, we suggest that the compressional segment of the conjugated strike-slip transition zone that was formed by the interaction of the WNW- and NNE-directed strike-slip faults was conducive to hydrocarbon accumulations.
Introduction
The North China block (NCB) is bounded by the Qinling-Dabie orogenic belt (QDOB) to the south and Yinshan–Yanshan orogenic belt to the north (Menzies and Xu, 1998; Zhao, 2001; Ren et al., 2002; Hu et al., 2006; Yang et al., 2008; Zhu et al., 2011; Wang et al., 2018b) (Figure 1A). Numerous faults with various orientations have developed since the Mesozoic in this area due to plate subduction, mantle upwelling, and lithospheric thinning. Previous studies have focused mainly on the NE-, NNE-, and nearly E-W-directed faults (Jia et al., 2021), while the WNW-directed faults have not been deeply studied. In particular, the distribution ranges and the formation mechanisms of the WNW-directed faults are still frequently debated (Li, et al., 2009; Suo, et al., 2013; Guo et al., 2015; Zhang, et al., 2017).
FIGURE 1
The Liaodong Bay subbasin is located in the northeastern Bohai Bay Basin (BBB), offshore China (Figure 1B) (Qi et al., 2008; Li L et al., 2012) and covers an area of more than 20,000 km2. The Liaodong Bay subbasin includes six ENE-oriented subunits and from west to east are the Liaoxinan uplift, Liaoxi sag, Liaoxi uplift, Liaozhong sag, and Liaodong uplift (Figure 1B) (Hsiao et al., 2004; Xu et al., 2015; Hu et al., 2018; Li et al., 2018; Liu L et al., 2019). The formation and evolution of this subbasin is mainly controlled by diverse faults, which have caused the most important tectonic deformations in this subbasin. Various fault types have developed in the LDB, which include extensional, strike-slip, and transtensional faults (Hu et al., 2018; Hu P et al., 2019; Hu Z W et al., 2019; Liu Y M et al., 2019). According to their orientations, the faults in the Liaodong Bay subbasin can be divided into three groups: NNE-directed, NE-directed, and NEE- or nearly E-W-directed, among which there are seven main NNE-directed faults, and the secondary fault directions are diverse (Cheng et al., 2015; Nan et al., 2015; Xu et al., 2015; Wu et al., 2016; Li et al., 2018).
The Yanshan orogenic belt (YOB) is located west of the Liaodong Bay subbasin. The western and central parts are characterized by nearly E-W- and WNW-directed compressional structures (Davis et al., 1998; Davis et al., 2001; Zhang et al., 2001; Ge et al., 2014; Wang et al., 2018a; Wang et al., 2018b), e.g., the Fengning-Longhua fault and Shangyi-Pingquan fault (Liu et al., 2004; Liu et al., 2018), and the Shangyi-Chongli-Chicheng fault (Zhang et al., 2006), which developed across Chengde, Luanping and Zhangjiakou Cities, Hebei Province, and Northern China.
In summary, although the research on the YOB (Davis et al., 2001; Zhang et al., 2001; Zhang et al., 2006; Cope et al., 2007; Zhang et al., 2011; Li et al., 2019; Li et al., 2021a) and Liaodong Bay subbasin (Cheng et al., 2015; Xu et al., 2015; Liu et al., 2016; Hu et al., 2018; Li et al., 2018; Li et al., 2021b) has achieved much progress and scientific understanding in previous studies, there are few results that are related to the origin of the WNW-directed faults. Regionally, the Liaodong Bay subbasin is located east of the YOB and is related to the E-W-directed tectonic system of the YOB in the extensional direction; thus, there may be an evolutionary and genetic relationship between them. It is suggested that the large-scale WNW-directed Zhangjiakou-Penglai Fault Zone (ZPFZ) developed north of the NCB and passes through the YOB, BBB, and Tan-Lu Fault Zone (TLFZ) (Wang et al., 2005; Suo et al., 2013; Guo et al., 2015; Peng et al., 2018). However, the ZPFZ traverses the middle of the BBB (Fu et al., 2004; Suo et al., 2013; Guo et al., 2015; Peng et al., 2018), and there have been no previous, relevant discussions regarding the WNW-directed fault system in the Liaodong Bay subbasin.
In this study, the fault system and stratigraphic features were explained in detail based on the latest 3-D seismic data. More importantly, WNW-directed fault systems were first recognized in the southern Liaodong Bay subbasin. The spatial geometries and temporal evolution processes were systematically investigated, and the genetic mechanisms were discussed. This study provides new evidence for the existence of the WNW-directed fault in the northern NCB and is conducive to clarifying the tectonic evolution and transition mechanism of the Liaodong Bay subbasin and even the entire eastern part of the NCB and will provide a reference for hydrocarbon exploration in the Liaodong Bay subbasin.
Geological Setting
The Liaodong Bay subbasin is located in the northeastern Bohai Sea, which is a part of the BBB, and is situated in eastern offshore China (Figure 1A) and consists of a Mesozoic-Cenozoic superimposed basin that developed on a Paleozoic platform (Chang, 1991; He and Wang, 2003; Qi, 2004; Qi and Yang, 2010; Zuo et al., 2011). The numerous faults in different regions of the Bohai Sea differ greatly in their orientations: (1) in the Bozhong subbasin, the faults mainly strike NE, NEE, and WNW (Sun et al., 2008); (2) in the Bodong subbasin, the faults mainly strike NNE, NE, and NEE (Wu et al., 2013); (3) in the Bonan subbasin, the faults mainly strike WNW, EW, and NNE (Zhang et al., 2017; Liu et al., 2020); and (4) in the Liaodong Bay subbasin, the faults mainly strike NNE and NE (Cheng et al., 2015; Li et al., 2015; Nan et al., 2015; Xu et al., 2015; Li et al., 2018; Hu et al., 2018) (Figure 1B). These faults with different directions controlled the formation and evolution of the Bohai Sea in the Mesozoic and Cenozoic and caused differences in basin architectures, hydrocarbon migration, and accumulation in different regions (Qi, 2004; Qi and Yang, 2010; Zuo et al., 2011; Li S et al., 2012).
The TLFZ traverses the eastern part of the Bohai Sea (Figure 1A) and now acts as a right-lateral strike-slip zone. It consists of several NNE-directed, steeper erect basement faults. The TLFZ controls the structural deformation and basin evolution of its interior and nearby areas and causes obvious transformations in these areas. The TLFZ exhibits obvious segmentation along the distribution direction in the Bohai Sea and can be divided into the Liaodong Bay segment, Bodong segment, and Bonan segment. From north to south, the TLFZ gradually widens, and the number of faults gradually increases (Deng, 2001; Hu et al., 2003; Wang et al., 2006; Gong et al., 2007; Wan et al., 2009).
The YOB is located north of the NCB and to the northwest of the Bohai Sea. It can extend westward to Baotou, Inner Mongolia, with a total length of over 1100 km (Xu and Liu, 2017). The YOB is characterized by folds and reverse faults, and the distribution directions of the structures are mainly E-W (in the west) and NE-NNE (in the east), with a gradual transition between them (Figure 1C) (Davis et al., 2001; Liu et al., 2004; Yang et al., 2006; Cope and Graham, 2007; Hu et al., 2010; Liu et al., 2015; Liu et al., 2018).
Since the Late Paleozoic, the NCB, where the Bohai Sea and YOB are located, has experienced plate subduction and continental collision in different directions (Menzies and Xu, 1998; Zhai and Liu, 2003; Zhu et al., 2011; Liu et al., 2013; Liu J et al., 2017; Liu et al., 2018). At the same time, it has been under the joint control of the Tethys tectonic domain, Paleo-Asian tectonic domain, and Paleo-Pacific tectonic domain (Chen, 1998; Dong et al., 2015; Wang et al., 2018a; Liu et al., 2021). The transformations and interactions of the three tectonic domains led to spatial and temporal differences at different stages between the regional dynamic background and local tectonic stress fields. In turn, these factors caused complex structural characteristics, evolution (Meng, 2003; Lin S Z et al., 2013; Meng et al., 2014; Dong et al., 2015; Liu S et al., 2017; Liu et al., 2018), and metamorphic core complexes (Liu et al., 2005; Lin et al., 2008; Davis and Darby, 2010; Wang et al., 2011; Ji et al., 2015; Zhu et al., 2015; Liu J et al., 2017).
Regarding the stratigraphic units, the LDB developed on the Archean and Paleoproterozoic metamorphic crystalline basement, which is consistent with the NCB. The overlying strata consist of Meso- to Neo-Proterozoic shallow sea carbonate and clastic sediments, Cambrian and Ordovician (Є + O) shallow sea carbonate and clastic sediments, Carboniferous and Permian (C + P) marine to continental transitional sediments, and Mesozoic and Cenozoic continental clastic sequences. Among these, the Mesozoic and Cenozoic deposits are mainly controlled by fault activity and can be subdivided into two mega-sequences. The Mesozoic mega-sequence can be divided into two sequences: the Jurassic (J) and Lower Cretaceous (K1) (Huang, 2019; Tong et al., 2019; Xi et al., 2019). The Triassic and Upper Cretaceous sequences are missing (Tong et al., 2019; Xi et al., 2019) (Figure 2). The Cenozoic is relatively complete in the Bohai Sea and includes Paleogene synrift and Neogene-Quaternary postrift mega-sequences (Hsiao et al., 2004; Cheng et al., 2015; Nan et al., 2015; Hu et al., 2018). The sediments that were deposited during the syn-rift stage are primary lacustrine formations, which include the Kongdian (Ek), Shahejie (Es), and Dongying (Ed) Formations, and the postrift stage is characterized by the deposition of the Guantao (Ng), Minghuazhen (Nm), and Pingyuan (Qp) Formations (Figure 2) (Hsiao et al., 2004; Hu et al., 2018).
FIGURE. 2
Data and Methods
This study is based on 3-D seismic reflection data that were provided by the Tianjin Oil Company Ltd., CNOOC (China National Offshore Oil Corporation). The 3-D seismic data include an intact seismic cube that was merged by the Tianjin Oil Company Ltd., CNOOC from several seismic cubes. The seismic cube covers an area of approximately 18,000 km2 with a line spacing of 12.5 m, and it images down to 6.0 s TWT. The 3-D seismic data were also processed by the companies introduced above by using calibrations with several deep wells.
A three-dimensional seismic interpretation was employed to identify and describe the geometry of the WNW-directed faults, and well logging and lithological data were also used to improve the correlations among the seismic reflectors and well data. This was followed by an interpretation of the main, regionally continuous seismic reflections and reflection terminations. The fault activity rate parameters and balanced cross-sections were used to determine the evolution of the WNW-directed faults.
Results
Geometric Characteristics of the WNW-Directed Faults in the Southern Liaodong Bay Subbasin
Detailed seismic data interpretations provide the basis for fault identification in petroliferous basins. Based on the detailed interpretation of the latest seismic data mentioned above, four WNW-directed faults were identified south of the LBD (Figure 3).
FIGURE 3
In this section, these WNW-directed faults mainly developed in the pre-Paleogene and deep Paleogene, with some extending to the Neogene. These WNW-directed faults are mostly characterized by low-angle listric normal faults, with great cutting depths and multiple cutting layers. In some segments, the WNW-directed faults and other secondary faults comprise multiple Y-shaped or negative flower-shaped structures (Figure 4), so we infer that these WNW-directed faults are probably transtensional faults. In addition, some of the WNW-directed faults are terminated by NE- or ENE-directed faults, which indicates that the WNW-directed faults formed earlier than the NE- or NEE-directed faults.
FIGURE 4
In the plane view, the seismic coherency time slices reveal that (1) the WNW-directed faults are discontinuous and are cut by the NNE-directed Lvda-21 Fault (LD21F) and Central Strike-slip Fault (CSF). (2) The WNW-directed faults are mainly distributed on both sides of the NNE-directed strike-slip faults. However, between the LD21F and CSF, those faults become N-S-directed. (3) The WNW-directed faults are relatively apparent at depth, with a parallel orientation. In the shallow layers, the WNW-directed faults were barely detected on both sides of the CSF and LD21F (Figure 5).
FIGURE 5
Stratigraphic Units Controlled by WNW-Directed Faults
The seismic reflection analysis shows that the strata controlled by the WNW-directed faults in the local area mainly include the Є + O, C + P, J, K1, and Ek to the fourth member of Es (Ek-Es4) and the third member of Es to Ed (Es3-Ed). The Є + O and C + P are characterized by continuous parallel high-amplitude seismic reflections, which gradually thin toward the WNW-directed faults (Figure 4). The Jurassic is characterized by mid-continuous high-amplitude seismic reflections, which gradually overlap and thin toward the WNW-striking faults (Figure 4). The Lower Cretaceous is characterized by basinward prograding discontinuous, low-amplitude chaotic seismic reflections that are thick and generally wedge-like, which gradually overlap and thin toward the WNW-striking faults (Figure 4). The Ek-Es4 sequence consists of chaotic, low-amplitude, discontinuous seismic reflections that are locally developed in the deep depression areas (Figures 4A,B). Es3-Ed is widely deposited in the LDB but in local areas, it is controlled by WNW-directed faults (Figure 4A).
In addition, the Jurassic-Paleozoic and Lower Cretaceous units exhibit two opposite wedges and when combined with the characteristics of the seismic reflections, suggest that WNW-directed faults may have undergone structural inversion.
Regional Geophysical Evidence for the Existence of WNW-Directed Faults in the Southern Liaodong Bay Subbasin
Apart from the properties indicated by the 3-D seismic reflection data, the Bouguer gravity anomalies, aeromagnetic anomalies, and crustal thicknesses also effectively reveal the existence of WNW-directed faults. (1) On the crustal thickness isopach map, along Chengde to Qinhuangdao, the contour trend changes from NE to NW. To the east of Qinhuangdao, two NE-trending Moho high values are separated (Figure 6A), and the separation belt extends southeast to Dalian. (2) On the Bouguer gravity anomaly map, the contour trend changes from NE to NW near Qinhuangdao. To the south of Qinhuangdao and Dalian, although the anomaly contours are complex, a NW-trending separation belt still exists (Figure 6B). (3) On the aeromagnetic anomaly map, NNE-NE-trending beading, such as positive anomaly zones, indicates the existence of the TLFZ (Figure 6C). On both sides of the NNE-NE-directed positive anomaly zone and south of Qinhuangdao and Dalian, the anomaly contours are clearly WNW-NW oriented.
FIGURE 6
Based on the above analysis, the presence of WNW-directed faults in the southern Liaodong Bay subbasin can be inferred. In previous studies, the Liaodong Bay subbasin and Bodong-Bozhong subbasin were thought to be separated by the WNW-directed Dalian-Qinhuangdao (Gong et al., 2007) or Qinhuangdao-Lvshun fault zone (Zhan et al., 2013), which contributed to confirming the existence of the WNW-directed faults in the southern Liadong Bay subbasin.
Discussion
Kinematics of the WNW-Directed Faults in the South Part of the Liaodong Bay Subbasin
Previous studies have suggested that the NNE- and NE-directed faults were the main basin-controlling faults in the Liaodong Bay subbasin, and their formation mechanism has been discussed in detail (Hsiao et al., 2004; Xu et al., 2015; Hu et al., 2018; Li et al., 2018). In contrast, the WNW-directed faults in the Liaodong Bay subbasin are rarely mentioned, which contain significant information regarding the regional tectonics. Therefore, an integrated investigation of the kinematics of the WNW-directed faults is overdue. By combining the dip-slip faulting rates, balanced cross-sections, and newly published geological evidence, the evolution of these faults and their coupling relationships to the surrounding plates were discussed.
Thrusting Stage During the Late Triassic and Jurassic
The WNW-directed faults were initiated during the Late Triassic of the Mesozoic era, and the negative fault activity rate suggests that these faults are reverse faults (Figures 7, 8H). Since the Middle Triassic, the Yangtze Plate has experienced the subduction of the southern Tethys Plate, which gradually strengthened in the Late Triassic (Lv et al., 2003; Hacker et al., 2009). This subduction event led to northward drifting of the Yangtze Plate, which ended up colliding with the NCB (Li et al., 2007; Li et al., 2013). After this collision, the Yangtze Plate continued to move northward with the NCB. Previously, the NCB collided and was spliced with the Siberian Plate during the Late Paleozoic, and the Mongolia-Okhotsk Ocean closed (Kravchinsky et al., 2002), so the northern margin of the NCB became a fixed boundary in the Late Triassic. From that time, the NCB experienced SSW- or SN-directed horizontal extrusion (Davis et al., 2001; Liu et al., 2012; Kim and Ree, 2013), which caused an overall uplift of the NCB that was accompanied by erosion of the Lower-Middle Triassic strata. Apatite fission track analysis of the samples from the Huanghua depression reveals uplift and cooling in the Late Triassic (239–200 Ma) and Jurassic (160–140 Ma) (Wu et al., 2020). The zircon shrimp dating of the inner-basin debris also shows 2 orogenic events in that period (Zhu et al., 2020). All the above results indicate a compressional stress field. Meanwhile, a series of compressional structures developed in the NCB, which included the embryonic form of WNW-directed faults that exhibited thrust faulting signatures.
FIGURE 7
FIGURE 8
During the Jurassic (196–136 Ma), the tectonic setting of eastern China transformed from the Tethys domain to the marginal Pacific domain; subsequently, Paleo-Pacific tectonics dominated the evolution of eastern China (Zhao et al., 2004; Zhang et al., 2007; Wang et al., 2018a). At that time, North China experienced a complicated convergent process between the Eurasian and Paleo-Pacific Plates, along with variations in the convergence directions, rates, and subduction angles of the slab. This dynamic background caused a weakened SSW or N-S horizontal contraction. New geochronological data reveal that the strata that were previously considered to be Late Jurassic should belong to the Early Cretaceous, which indicates that the Jurassic strata in the study area were deposited earlier than ∼136 Ma (Zhang et al., 2019). As a result, the NCB experienced intracontinental deformation, and the WNW-directed faults in the Liaodong Bay subbasin retained their reverse faulting characteristics (Figures 7, 8G, 9B). Consequently, the region evolved into a fold-thrust belt-induced flexural basin system and a high-standing block (horst)-rift-basin system (Liu S et al., 2017), which is consistent with the contemporaneous development of thrust nappe structures and molasse formation (Dong et al., 2013).
FIGURE 9
Extension Stage During the Early Cretaceous
The tectonic contraction in the Jurassic extended into the earliest Early Cretaceous (Meng, 2003; Liu J et al., 2017) and from approximately 136 Ma, the regime changed to extension (Cheng et al., 2018). Lithospheric thinning occurred underneath the NCB (Yang, 2003; Zhai et al., 2007; Zhu et al., 2011; Wu et al., 2014) and led to the formation of widespread and intensive extensional structures (Figure 9C). Meanwhile, some metamorphic core complexes and extensional domes developed in Yanshan and southern Liaoning Provinces, such as the Fangshan magma dome (Shan et al., 2006; Yan et al., 2006), Yunmengshan core complex (Zhu et al., 2015), Kalaqin extensional dome (Lin et al., 2014), Waziyu core complex (Zhang et al., 2012), and Linglong extensional dome (Lin W et al., 2013). The isotopic ages of these structures are constrained to between 135 and 129 Ma. Analysis of volcanic rocks and debris in the BBB also shows that there were 2 ages of volcanic rocks (e.g., 125–120 Ma and 110–100 Ma)., which indicated that regional extension occurred in the Early Cretaceous. In addition, the NNE-directed TLFZ experienced large-scale sinistral shear at the beginning of the Early Cretaceous (Zhu et al., 2005), which could have been derived from NNE- or SN-directed extension. Under the joint control of the deep dynamic background and shallow NNE-directed extension derived from the left-lateral movement of the TLFZ, the early WNW-directed faults were transformed into normal faults, with large amounts of displacement (Figures 7, 8F, 9C).
Thrusting Stage During the Late Cretaceous
During the Late Cretaceous (93.9–65 Ma), a new lithospheric mantle formed under the NCB (Wu et al., 2014). The gravitational influence of the newly formed lithosphere caused contraction of the shallow crust and thus superimposed the compression on the early extensional fault basin (Ying et al., 2006). At the same time, the Izanagi Plate in the Western Pacific Ocean was completely subducted under the Eurasian Plate in the Late Cretaceous (85 Ma), and the WNW-ward subduction of the Kula Plate (Zhang et al., 2008) caused the transformation of the regional stress field in the NCB into nearly NW-SE compression (Li S Z et al., 2005; Li W et al., 2005). Thus, the Early Cretaceous extensional fault basins were inverted under the regional contraction regime. A certain number of reverse faults and folds developed, such as the Chengbei-20 Fault in the Jiyang depression and Cangxian uplift in the Huanghua depression (Zhou et al., 2003; Li and Gao, 2010; Li et al., 2021a). In the study area, the WNW-directed faults ceased their normal faulting motions, and some local segments were transformed into thrust faults (Figure 8E). From a regional tectonics standpoint, this interpretation is also evidenced by a regional tectonic inversion event that occurred between 90 and 65 Ma in the Hailaer, Songliao, and Sanjiang Basins in Northeast China (Liu S et al., 2017; Liu et al., 2020). Meanwhile, this event is synchronous with the extensive fold development and striking angular unconformity within most of East Asia (Liu et al., 2020), which demonstrates an extensive compressional deformation history during the Late Cretaceous.
Reactivation and Extension Stage During the Cenozoic
During the Paleogene (66–23 Ma), deep mantle upwelling caused extension in the shallow crust, and the WNW-directed faults were reactivated locally.
During the depositional period of the Ek-Es4 sequence (e.g., Paleocene to Early Eocene), the motion along the TLFZ still consisted of sinistral shear (Hu et al., 2003). Some pre-existing WNW-directed faults were reactivated and controlled the lacustrine deposition (Figures 7, 8D, 9D), which indicates the inheritance of the Early Cretaceous tectonics (Hou and Hari, 2014). In addition, the main WNW-directed faults in the middle part of the BBB have similar characteristics, such as the Jiyang subbasin (Cheng et al., 2018; Liu et al., 2020), Chengbei subbasin (Liu L et al., 2019), and Huanghekou and Laizhouwan subbasins (Zhang et al., 2017), which reflect the prevalence of WNW-directed fault inheritance and reactivation during the Paleocene to early Eocene.
Since the Middle Eocene (the depositional period of the Es3-Ed sequence), the subduction direction of the Pacific Plate changed to WNW-directed, and the motion of the TLFZ then transformed into dextral shear (Zhu et al., 2021), which was derived from NW-directed extension and NE-directed compression. Since the direction of the derived compression was vertical to the WNW-directed faults, the activity of the WNW-directed faults weakened and gradually stopped (Figures 7, 8B,C, 9E). Instead, NNE-directed faults began to activate and became the main basin-controlling faults in the Liaodong Bay subbasin (Hu et al., 2003). Consequently, the NNE- and NE-directed faults cut across the WNW-directed faults and reconstructed the previous tectonic patterns (Figure 9E). Additionally, due to the right-lateral strike-slips of the NNE-directed faults, the strikes of the WNW-directed faults between the Lvda21 and Central Strike-slip faults changed in the N-S direction (Figures 3 and 5). Similar to the study area, in the Zhanhua subbasin and Chengbei subbasin in the southeastern BBB, the strikes of the Mesozoic basin-controlling WNW-directed faults also changed to the N-S direction due to the close distance to the TLFZ (Li et al., 2006; Cheng et al., 2015).
During the depositional period of the Neogene-Quaternary sequence (e.g., Miocene-Holocene), the Bohai Sea area entered a postrift thermal subsidence stage, and the subsidence center migrated to the Bozhong sag (Figure 9F). Since the depositional period of the upper Minghuazhen subsequence, regional N-S extension (Li L et al., 2012) caused the WNW-directed faults to reactivate (Suo et al., 2013), and the motion was extensional with a sinistral shear sense.
Implications for the Distribution of the WNW-Directed Fault System in the Northern Part of the NCB
When compared with the NNE- and NE-directed faults, WNW-directed faults are not obvious in eastern China and are generally distributed in a dispersed manner (Suo et al., 2013). Previous studies have suggested that a large-scale WNW-directed fault zone developed in the northern NCB, namely, the Zhangjiakou-Penglai Fault Zone (Gao et al., 2001; Xu et al., 2012; Suo et al., 2013) or Zhangjiakou-Bohai Fault Zone (Lai et al., 2004), which is composed of many NW-, WNW-, and nearly E-W-directed faults. These faults in the ZPFZ have mutual cutting relationships with the nearly N-S- and NNE-directed faults. The ZPFZ can be divided into an onshore part in the west and offshore part in the east. The onshore part includes the Zhangjiakou-HuaiLai section and Beijing-Tianjin section, and both of them are located south of the Shangyi-Chicheng-Chongli fault, which is the western section of the southern boundary fault of the YOB (Zhang et al., 2011) (Figure 1). The offshore part includes the Bohai section located in the Bohai Sea and Penglai-Weihai section located in the north part of the Shandong Peninsula, and the Bohai section is mainly composed of the Weibei fault, Sha’nan fault, Huanghekou fault, and Laibei fault, all of which are located in the middle of the Bohai Sea area (Gao et al., 2001).
The Liaodong Bay subbasin is in the northern Bohai Sea, while few studies have been conducted on the WNW-directed faults. Based on the regional geophysical data and the offset of the NNE- and NE-directed TLFZ, it is suggested that a WNW-directed fault zone may have developed between the Liaodong Bay subbasin and Bodong-Bozhong subbasin, which is called the Qinhuangdao-Lvshun fault zone (Qi et al., 2004; Li and Hou, 2019). Based on the analysis in this study, we speculate that the WNW-directed faults in the south part of the Liaodong Bay subbasin should extend westward to the YOB and connect inland with the Shangyi-Pingquan fault.
However, the fault properties of the YOB are significantly different from the extensional deformations in the offshore basins. The nearly E-W- and WNW-directed faults in the YOB are generally considered to be reverse faults (Davis et al., 2001; Zhang et al., 2001; Zhang et al., 2011; Cope et al., 2007), while the Liaodong Bay subbasin is typically considered to be a strike-slip and extensional basin (e.g., Wenxian). The differences in the tectonic properties led to a lack of attention to the WNW-directed faults in the study area. In this study, we find that although the WNW-directed faults in the Liaodong Bay subbasin were mainly extensional and strike-slip in the Cenozoic, they had been reversed faults during the Late Triassic and Jurassic (Figures 7, 8G,H), which are consistent with the nearly E-W- and WNW-directed faults in the YOB. The nearly E-W- and WNW-directed reverse faults in the YOB mainly acted during the Mesozoic (Davis et al., 2001; Zhang et al., 2001; Cope et al., 2007; Zhang et al., 2011) and being affected by continuous uplift during the Cenozoic, these faults ceased being active. Based on the above analysis, we speculate that the formation mechanism and evolution of the WNW-directed faults in the Liaodong Bay subbasin are similar to those in the YOB. In addition to the ZPFZ, another nearly WNW-directed fault zone should be present in the northern NCB along Jining-Shangyi-Pingquan and Qinhuangdao-Lvshun.
Implications for Hydrocarbon Exploration in the Southern Liaodong Bay Subbasin
Previous exploration efforts have confirmed the potential for oil and gas accumulations in the southern Liaodong Bay subbasin (Jia et al., 2018). The oil-source correlation analysis shows that these oils were derived from the source rocks of the Es1 and Ed3 strata. Hydrocarbon migration and accumulation primarily occurred during the depositional period of the Ed and N + Q sequences (Xu et al., 2011; Wang et al., 2014; Teng et al., 2016). As one of the hydrocarbon-rich depressions in the Bohai Sea, the Liaodong Bay subbasin has witnessed discoveries of several large and medium oil and gas fields, such as LD27, LD21, and LD16. After decades of exploration, the level of oil and gas exploration of the Paleogene reservoir in the Bohai Sea has been relatively high, and the pre-Paleogene reservoir is now the focus and hotspot of exploration in the BBB (Tong et al., 2012; Zhao et al., 2015; Xu et al., 2019). To date, hydrocarbon accumulations in the volcanic rocks of the Mesozoic and carbonates in the Paleozoic have been found in the Liaodong Bay subbasin, north of the BBB. However, until now, only 10 buried hill reservoirs have been discovered in the Bohai Sea (Deng, 2015), and the degree of exploration is significantly lower than that of the Cenozoic.
In this study, the WNW-directed faults that formed in the Mesozoic were discovered south of the Liaodong Bay subbasin. In addition, the residual strata of the Mesozoic and Paleozoic were revealed based on their seismic reflection characteristics. Thus, we speculate that the southern Liaodong Bay subbasin has a stratigraphic basis for the formation of buried hills. Moreover, the multistage reverse movements along the WNW-directed faults caused the formation of multiple angular unconformities during the uplift and erosion stages, which significantly improved the physical reservoir properties (Tian and Jiang, 2008). These tectonic activities simultaneously resulted in the formation of effective traps (Figures 4 and 10). In terms of hydrocarbon migration, the unconformities provide long-term continuous migration pathways (Zhao et al., 2015). Oil and gas can migrate from the hydrocarbon generation centers to the highpoints of the buried hills through extensional faults and these key unconformities. In addition, the late, active NNE-directed strike-slip faults can effectively seal the oil and gas accumulations. Based on the aforementioned analysis, buried Mesozoic and Paleozoic hills can be the subsequent exploration domain in the future (Figure 10).
FIGURE10
Another issue worthy of attention is the distribution of oil and gas in the study area. At present, it is believed that oil and gas accumulations are abundant along the TLFZ, which has been confirmed by the exploration results (Gong et al., 2007; Zhu et al., 2019). However, drilling failures occurred during the exploration of structural traps along the TLFZ. Previous research has revealed the superior genetic potential of the source rocks in the southern part of the LBD (Huang et al., 2013). The key factor for hydrocarbon accumulations is whether there are effective traps and sealing faults. The NNE-directed strike-slip faults in the southern part of the LBD did not have a simple linear distribution but were slightly bending (Figures 3 and 5). The Late Paleogene to Neogene was a key period for oil accumulation. When the NNE-directed strike-slip faults mainly exhibited dextral shear, the WNW-directed faults exhibited sinistral shear (Suo et al., 2013; Peng et al., 2018). These two sets of strike-slip faults with conjugate strikes and opposite patterns simultaneously formed a conjugate strike-slip transition zone (Figure 10). Both the bending and the conjugation of the main strike-slip faults could result in local extension and compression, between which compression was conducive to the formation of fault gouges, so the permeabilities were lower, which contributed to the preservation of oil and gas (Wang et al., 2016). Previous studies have suggested that compressional strike-slip transfer zones or strike-slip derived structures are favorable locations for hydrocarbon accumulations and could therefore easily form large- and medium-sized oil and gas reservoirs (Xu, 2016). Therefore, in future exploration efforts, not only fine-scale seismic interpretations but also local stress field analyses are required, especially in the locations of extensional and compressional zones, which should be specified.
Conclusion
1) Four WNW-directed faults developed south of the Liaodong Bay subbasin and are mainly distributed on both sides of NNE-directed strike-slip faults, with poor continuity and parallel orientations and controlled the deposition of the Jurassic and Lower Cretaceous strata of the Mesozoic and Ek-Es4 of the Cenozoic. Between the two NNE-directed strike-slip faults, the faults controlling the Mesozoic and Ek-Es4 are nearly N-S-directed instead of WNW-directed.
2) The WNW-directed faults in the south part of the Liaodong Bay subbasin initially were reverse faults beginning in the Late Triassic. During the Jurassic, these reverse WNW-directed faults became less active. The WNW-directed faults transformed into normal faults in the Early Cretaceous with intensive activity. During the Cenozoic, the WNW-directed faults were reactivated as normal faults during the depositional period of the Ek-Es4 sequence and then gradually became inactive.
3) The formation mechanism and evolution of the WNW-directed faults in the Liaodong Bay subbasin are similar to those in the YOB. In addition to the ZPFZ, another nearly E-W- and WNW-directed fault zone should be developed in the northern part of the NCB along Jining-Shangyi-Pingquan and Qinhuangdao-Lvshun.
4) The development of WNW-directed faults in the southern Liaodong Bay subbasin is conducive to the formation of buried Mesozoic and Paleozoic hills and hydrocarbon accumulations. In addition, we suggest that the compressional segment of the conjugated strike-slip transition zone that formed by the interaction of the WNW- and NNE-directed strike-slip faults is conducive to hydrocarbon accumulations.
Statements
Data availability statement
The raw data supporting the conclusions of this article will be made available by the authors, without undue reservation.
Author contributions
W.L.: Conceptualization, methodology, writing-original draft; M.M. and T.Z.: Methodology, software, writing-reviewing and editing; X.C., Y.L., and D.W.: Revising the manuscript critically for important intellectual content; C.N. and H.Y.: Acquisition of data; supervision.
Funding
This study was funded by grants from the Ministry of Science and Technology of China (2016ZX05006-007 and 2016ZX05024-002). We thank the TianJin Oil Company, Ltd., CNOOC, and individuals who contributed the seismic data for this work.
Conflict of interest
Author ZT, NC and YH are employed by CNOOC.
The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Publisher’s note
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors, and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.
References
1
ChenA. (1998). Geometric and Kinematic Evolution of Basement-Cored Structures: Intraplate Orogenesis within the Yanshan Orogen, Northern China. Tectonophysics292 (1-2), 17–42. 10.1016/s0040-1951(98)00062-6
2
ChengY.WuZ.LuS.LiX.LinC.HuangZ.et al (2018). Mesozoic to Cenozoic Tectonic Transition Process in Zhanhua Sag, Bohai Bay Basin, East China. Tectonophysics730, 11–28. 10.1016/j.tecto.2018.02.010
3
ChengY.WuZ.YanS.XuC.LiW.ZhangJ.et al (2015). Cenozoic Tectonic Evolution of Liaodong Dome, Northeast Liaodong Bay, Bohai, Offshore China, Constraints from Seismic Stratigraphy, Vitrinite Reflectance and Apatite Fission Track Data. Tectonophysics659, 152–165. 10.1016/j.tecto.2015.07.039
4
Cheng-yong ChangC. Y. (1991). Geological Characteristics and Distribution Patterns of Hydrocarbon Deposits in the Bohai Bay Basin, east China. Mar. Pet. Geology.8 (1), 98–106. 10.1016/0264-8172(91)90048-6
5
CopeT. D.GrahamS. A. (2007). Upper Crustal Response to Mesozoic Tectonism in Western Liaoning, North China, and Implications for Lithospheric Delamination. Geol. Soc. Lond. Spec. Publications280 (1), 201–222. 10.1144/SP280.10
6
CopeT. D.ShultzM. R.GrahamS. A. (2007). Detrital Record of Mesozoic Shortening in the Yanshan belt, NE China: Testing Structural Interpretations with basin Analysis. Basin Res.19 (2), 253–272. 10.1111/j.1365-2117.2007.00321.x
7
DavisG. A.CongW.YadongZ.JinjiangZ.ChanghouZ.GehrelsG. E. (1998). The Enigmatic Yinshan Fold-And-Thrust belt of Northern China: New Views on its Intraplate Contractional Styles. Geol26 (1), 43–46. 10.1130/0091-7613(1998)026<0043:teyfat>2.3.co;2
8
DavisG. A.DarbyB. J. (2010). Early Cretaceous Overprinting of the Mesozoic Daqing Shan Fold-And-Thrust belt by the Hohhot Metamorphic Core Complex, Inner Mongolia, China. Geosci. Front.1 (1), 1–20. 10.1016/j.gsf.2010.08.001
9
DavisG. A.YadongZ.CongW.DarbyB. J.ChanghouZ.GehrelsG. (2001). Mesozoic Tectonic Evolution of the Yanshan Fold and Thrust belt, with Emphasis on Hebei and Liaoning Provinces, Northern China. Paleozoic Mesozoic Tectonic Evol. Cent. East. Asia: Continental Assembly Intracontinental Deformation.10.1130/0-8137-1194-0.171
10
DengY. H. (2001). Control of the NeotectonismAalong Tancheng-Lujiang Fracture Zone on Hydrocarbon Accumulationin the Eastern Bohai Sea. China Offshore Oil and Gas05, 301–305. (in Chinese). 0.2001-05-000.
11
DengY. H. (2015). Formation Mechanism and Exploration Practice of Large-Medium Buried-hill Oil fields in Bohai Sea. Acta Petrolei Sinica36 (3), 253–261. (in Chinese). 10.7623/syxb201503001
12
DongS.GaoR.YinA.GuoT.ZhangY.HuJ.et al (2013). What Drove Continued Continent-Continent Convergence after Ocean Closure? Insights from High-Resolution Seismic-Reflection Profiling across the Daba Shan in central China. Geology41, 671–674. 10.1130/g34161.1
13
DongS.ZhangY.LiH.ShiW.XueH.LiJ.et al (2018). The Yanshan Orogeny and Late Mesozoic Multi-Plate Convergence in East Asia-Commemorating 90th Years of the "Yanshan Orogeny". Sci. China Earth Sci.61, 1888–1909. 10.1007/s11430-017-9297-y
14
DongS.ZhangY.ZhangF.CuiJ.ChenX.ZhangS.et al (2015). Late Jurassic-Early Cretaceous continental Convergence and Intracontinental Orogenesis in East Asia: A Synthesis of the Yanshan Revolution. J. Asian Earth Sci.114, 750–770. 10.1016/j.jseaes.2015.08.011
15
FengC. J.ZhangP.MengJ. (2017). In Situ stress Measurement at Deep Boreholes along the Tanlu Fault Zone and its Seismological and Geological Significance. Prog. Geophys.32, 946–967. (in Chinese).
16
FuZ.LiuJ.LiuG. (2004). On the Long-Term Seismic hazard Analysis in the Zhangjiakou-Penglai Seismotectonic Zone, China. Tectonophysics390 (1-4), 75–83. 10.1016/j.tecto.2004.03.021
17
GaoZ. W.XuJ.SongC. Q.et al (2001). The Segmental Character of Zhangjiakou-Penglai Fault. North China Earthquake Sci.19 (1), 35–42. (in Chinese).
18
GeX. H.LiuJ. L.RenS. M.et al (2014). The Formation and Evolution of the Mesozoic-Cenozoic continental Tectonics in Eastern China. Geology. China41 (1), 19–38. (in Chinese).
19
GongZ. S.CaiD. S.ZhangG. C. (2007). Dominating Action of Tanlu Fault on Hydrocarbon Accumulation in Eastern Bohai Sea Area [J]. Acta Petrolei Sinica28 (4), 1. (in Chinese). 10.1016/S1872-5813(07)60034-6
20
GuoL.LiS.SuoY.JiY.DaiL.YuS.et al (2015). Experimental Study and Active Tectonics on the Zhangjiakou-Penglai Fault Zone across North China. J. Asian Earth Sci.114 (DEC.15PT.1), 18–27. 10.1016/j.jseaes.2015.03.045
21
HackerB. R.WallisS. R.McWilliamsM. O.GansP. B. (2009). 40Ar/39Ar Constraints on the Tectonic History and Architecture of the Ultrahigh-Pressure Sulu Orogen. J. Metamorphic Geoloy27 (9), 827–844. 10.1111/j.1525-1314.2009.00840.x
22
HeL. J.WangJ. Y. (2003). Cenozoic thermal History of the Bohai Bay Basin: Constraints from Heat Flow and Coupled basin–mountain Modeling. Phys. Chem. Earth, Parts A/B/C28 (9-11), 421–429. 10.1016/s1474-7065(03)00062-7
23
HouG.HariK. R. (2014). Mesozoic-Cenozoic Extension of the Bohai Sea: Contribution to the Destruction of North China Craton. Front. Earth Sci.8 (2), 202–215. 10.1007/s11707-014-0413-3
24
HouG.WangY.HariK. R. (2010). The Late Triassic and Late Jurassic Stress fields and Tectonic Transmission of North China Craton. J. Geodynamics50 (3-4), 318–324. 10.1016/j.jog.2009.11.007
25
HsiaoL.-Y.GrahamS. A.TilanderN. (2004). Seismic Reflection Imaging of a Major Strike-Slip Fault Zone in a Rift System: Paleogene Structure and Evolution of the Tan-Lu Fault System, Liaodong Bay, Bohai, Offshore China. Bulletin88 (1), 71–97. 10.1306/09090302019
26
HuJ.ZhaoY.LiuX.XuG. (2010). Early Mesozoic Deformations of the Eastern Yanshan Thrust belt, Northern China. Int. J. Earth Sci. (Geol Rundsch)99 (4), 785–800. 10.1007/s00531-009-0417-5
27
HuP.YangF.TianL.WuK.WangW. (2019). Stress Field Modelling of the Late Oligocene Tectonic Inversion in the Liaodong Bay Subbasin, Bohai Bay Basin (Northern China): Implications for Geodynamics and Petroleum Accumulation. J. Geodynamics126, 32–45. 10.1016/J.JOG.2019.01.003
28
HuP.YangF.WangW.XuC.ZhangR.HuY.et al (2018). Thermal Anomaly Profiles Inferred from Fluid Inclusions Near Extensional and Strike-Slip Faults of the Liaodong Bay Subbasin, Bohai Bay Basin, China: Implications for Fluid Flow and the Petroleum System. Mar. Pet. Geology.93, 520–538. 10.1016/J.MARPETGEO.2018.03.035
29
HuS.RazaA.MinK.KohnB. P.ReinersP. W.KetchamR. A.et al (2006). Late Mesozoic and Cenozoic Thermotectonic Evolution along a Transect from the north China Craton through the Qinling Orogen into the Yangtze Craton, central China. Tectonics25, a–n. 10.1029/2006TC001985
30
HuW. S.LvB. Q.GuanD. Y.et al (2003). Characteristics of Tanlu Fault Zone and Development of Mesozoic and Cenozoic Basins along it. Mar. Geology. Quat. Geology.23 (4), 51–58.
31
HuZ. W.XuC. G.WangD. Y.et al (2019). Superimposed Characteristics and Genetic Mechanism of Strike-Slip Faults in the Bohai Sea, China. Pet. Exploration Dev.46 (02), 63–77. 10.1016/s1876-3804(19)60007-8
32
HuangD. Y. (2019). Jurassic Integrative Stratigraphy and Timescale of China. Sci. China Earth Sci.62 (01), 227–259. 10.1007/s11430-017-9268-7
33
HuangX. B.XuC. G.ZhouX. H. (2013). Hydrocarbon Distribution Characteristics and Accumulation Period of Second Member of Dongying Formation in the South of Liaozhong Sag. Pet. Geology. Engneering27 (4), 16–19. (in Chinese). 10.3969/j.issn.1673-8217.2013.04.005
34
JiM.LiuJ.HuL.ShenL.GuanH. (2015). Evolving Magma Sources during continental Lithospheric Extension: Insights from the Liaonan Metamorphic Core Complex, Eastern North China Craton. Tectonophysics647-648, 48–62. 10.1016/j.tecto.2015.01.023
35
JiaN.LiuC. Y.ZhangG. C.LeiH. (2015). Cenozoic Multiple Faulting and Tecnotic Evolution in the Liaodong Bay Depression. Chin. J. Geology. (Scientia Geologica Sinica)50 (2), 377–390. (in Chinese). 10.3969/j.issn.0563-5020.2015.02.003
36
JiaN.LiuC.ZhouL. (2018). Characteristics of Fault Structure and its Control on Hydrocarbons in the Liaodong Bay Depression[J]. J. Northwest University(Natural Sci. Edition)48 (06), 839–849.
37
JiaN.HuangL.LiuC.LiD.XuC. (2021). Differential Faulting in a Narrow Rift basin Influenced by Synchronous Strike-Slip Motion: The Liaodong Bay sub-basin, Offshore Bohai Bay Basin, China. Mar. Pet. Geology.124, 104853. 10.1016/j.marpetgeo.2020.104853
38
KimH. S.ReeJ.-H. (2013). Permo-Triassic Changes in Bulk Crustal Shortening Direction during Deformation and Metamorphism of the Taebaeksan Basin, South Korea Using Foliation Intersection/inflection Axes: Implications for Tectonic Movement at the Eastern Margin of Eurasia during the Songrim (Indosinian) Orogeny. Tectonophysics587, 133–145. 10.1016/j.tecto.2012.08.033
39
KravchinskyV. A.CogneJ.-P.HarbertW. P.KuzminM. I. (2002). Evolution of the Mongol-Okhotsk Ocean as Constrained by New Palaeomagnetic Data from the Mongol-Okhotsk Suture Zone, Siberia. Geophys. J. Int.148 (1), 34–57. 10.1046/j.1365-246x.2002.01557.x
40
KuskyT. M.LiJ. (2003). Paleoproterozoic Tectonic Evolution of the North China Craton. J. Asian Earth Sci.22 (4), 383–397. 10.1016/s1367-9120(03)00071-3
41
KuskyT. M.WindleyB. F.ZhaiM.-G. (2007). Tectonic Evolution of the North China Block: From Orogen to Craton to Orogen. Geol. Soc. Lond. Spec. Publications280 (1), 1–34. 10.1144/SP280.1
42
LaiX.-L.ZhangX.-K.ChengS.-X.FangS.-M. (2004). Study on Crust-Mantle Transitional Zone in West Margin of Zhangjiakou-Bohai Fault Belt. Chin. J. Geophys.47 (5), 900–907. 10.1002/cjg2.567
43
LiJ.HouG. (2019). Stress Development in Heterogeneous Lithosphere: Insights into Earthquake Initiation in the Tan-Lu Fault Zone. Tectonophysics750, 329–343. 10.1016/j.tecto.2018.11.018
44
LiJ.ZhangY.DongS.ShiW. (2013). Structural and Geochronological Constraints on the Mesozoic Tectonic Evolution of the North Dabashan Zone, South Qinling, central China. J. Asian Earth Sci.64 (Mar.5), 99–114. 10.1016/j.jseaes.2012.12.001
45
LiL.ZhongD. L.YangC. C. (2012). Extension Order and its Deep Geological Background: Evidence from Western Shandong Rise and Jiyang Depression in the Late Mesozoic-Cenozoic. Earth Sci. Front.19 (5), 255–273. (in Chinese).
46
LiL.ZhongD. (2018). Tectonic Uplift Recorded by Detrital Zircon Fission Track Age in Jiyang Depression, Bohai Bay Basin. Acta Petrologica Sinica34, 483–494. (in Chinese).
47
LiS. Z.WangJ. D.LiuJ. Z. (2005). Mesozoic Structure and its Tectonic Setting in the Western Shandong Block. Acta Geologica Sinica79 (4), 487–497. (in Chinese). 10.3321/j.issn:0001-5717.2005.04.006
48
LiS.KuskyT. M.WangL.ZhangG.LaiS.LiuX.et al (2007). Collision Leading to Multiple-Stage Large-Scale Extrusion in the Qinling Orogen: Insights from the Mianlue Suture. Gondwana Res.12 (1-2), 121–143. 10.1016/j.gr.2006.11.011
49
LiS.ZhaoG.DaiL.ZhouL.LiuX.SuoY.et al (2012). Cenozoic Faulting of the Bohai Bay Basin and its Bearing on the Destruction of the Eastern North China Craton. J. Asian Earth Sci.47, 80–93. 10.1016/j.jseaes.2011.06.011
50
LiW.GaoR. S. (2010). Development Characteristics of Positive Inversion Tectonics and its Controlling to Hydrocarbon Accumulation in Jiyang Depression. China Pet. Exploration15 (5), 17–22. (in Chinese). 10.3969/j.issn.1672-7703.2010.05.004
51
LiW.GuoT. T.WuZ. P. (2019). Application of Balanced Cross-Section Method in Extension, Strike-Slip Superposition and Ratio Analysis: A Case Study of Liaodong Bay Depression, Bohai Bay Basin. Geol. Rev.65 (06), 1501–1514.
52
LiW.MengM. F.ChenX. P. (2021b). Quantitative Characterization of Extension and Compression Derived from Bending Strike-Slip Faults and Their Petroleum Geological Significance of the Eastern Bohai Sea. J. China Univ. Petroleum(Edition Nat. Science)45 (05), 23–32.
53
LiW.PingM. M.ZhouD. H. (2018). Estimation of the Cenozoic Strike-Slip Displacement for Major Faults in the Liaodong Bay Depression and its Geological Significance. Geotectonica et Metallogenia42 (03), 445–454.
54
LiW.RenJ.LiuY. (2015). Development and Formation Mechanism of Cenozoic Tectonics in the East Area of Liaodong Bay Depression. Geol. Sci. Tech. Inf.34 (006), 63–69. (in Chinese). 0.2015-06-008.
55
LiW.WuZ. P.LiuH. (2009). Mesozoic and Cenozoic basin Evolution and Coal-Derived Gas Accumulation of Upper Paleozoic in the Area of Bohai Bay Basin. Pet. Geology. Recovery Efficiency16 (1), 13–16. (in Chinese). 10.3969/j.issn.1009-9603.2009.01.004
56
LiW.WuZ. P.ZhangM. H. (2006). Development Characteristic of Mesozoic and Cenozoic Faults and its Control over Deposition in Chengdao Area. J. China Univ. Pet. (Edition Nat. Science)30 (1), 1–6+11. (in Chinese). 10.3321/j.issn:1000-5870.2006.01.001
57
LiW.WuZ. P.ZhouY. Q. (2005). Reconstruction of the Thickness of the Mesozoic Strata and Mesozoic Proto-type Basin in the Jiyang Depression. Geol. Rev.51 (05), 507–516. (in Chinese). 10.3321/j.issn:0371-5736.2005.05.004
58
LiW.JiaH.WuZ.NiuC.ChenX. (2021a). Controls of Strike-Slip Faults on Geomorphology and Sediment Dispersal in the Paleogene Bohai Bay Area-From a Source to Sink Perspective. Mar. Pet. Geology.126, 104946. 10.1016/j.marpetgeo.2021.104946
59
LinS. Z.ZhuG.YanL. J. (2013). Discussion on Uplifting Mechanism of the Linglong Batholith in Eastern Shandong. Geol. Rev.59 (5), 832–844. (in Chinese). 10.3969/j.issn.0371-5736.2013.05.004
60
LinS.ZhaoT.SongL.ZhuG.LiuB. (2014). Structural Characteristics and Formation Mechanism of the Kalaqin Metamorphic Core Complex in the Yanshan Area, China. Chin. Sci. Bull.59, 3174–3189. (in Chinese). 10.1360/n972014-00100
61
LinW.CharlesN.ChenY.ChenK.FaureM.WuL.et al (2013). Late Mesozoic Compressional to Extensional Tectonics in the Yiwulüshan Massif, NE China and Their Bearing on the Yinshan-Yanshan Orogenic belt. Gondwana Res.23 (1), 78–94. 10.1016/j.gr.2012.02.012
62
LinW.FaureM.MoniéP.SchärerU.PanisD. (2008). Mesozoic Extensional Tectonics in Eastern Asia: The South Liaodong Peninsula Metamorphic Core Complex (NE China). J. Geology.116 (2), 134–154. 10.1086/527456
63
LiuJ.DavisG. A.LinZ.WuF. (2005). The Liaonan Metamorphic Core Complex, Southeastern Liaoning Province, North China: A Likely Contributor to Cretaceous Rotation of Eastern Liaoning, Korea and Contiguous Areas. Tectonophysics407 (1-2), 65–80. 10.1016/j.tecto.2005.07.001
64
LiuJ.GanH.JiangH.ZhangJ. (2017). Rheology of the Middle Crust under Tectonic Extension: Insights from the Jinzhou Detachment Fault Zone of the Liaonan Metamorphic Core Complex, Eastern North China Craton. J. Asian Earth Sci.139 (May 15), 61–70. 10.1016/j.jseaes.2016.12.024
65
LiuJ.ZhaoY.LiuA.YeH. (2015). Late Jurassic to Early Cretaceous Sedimentary-Tectonic Development in the Chengde Basin, Yanshan Fold-Thrust belt, North China Craton. J. Asian Earth Sci.114 (DEC.15PT.4), 611–622. 10.1016/J.JSEAES.2014.08.019
66
LiuJ.ZhaoY.LiuX.WangY.LiuX. (2012). Rapid Exhumation of Basement Rocks along the Northern Margin of the North China Craton in the Early Jurassic: Evidence from the Xiabancheng Basin, Yanshan Tectonic Belt. Basin Res.24 (5), 544–558. 10.1111/j.1365-2117.2011.00538.x
67
LiuL.ChenH.WangJ.ZhongY.DuX.GanX.et al (2019). Geomorphological Evolution and Sediment Dispersal Processes in Strike-Slip and Extensional Composite Basins: A Case Study in the Liaodong Bay Depression, Bohai Bay Basin, China. Mar. Pet. Geology.110, 73–90. 10.1016/J.MARPETGEO.2019.07.023
68
LiuL.ZhongY.ChenH.XuC.WuK. (2016). Seismically Induced Soft-Sediment Deformation Structures in the Palaeogene Deposits of the Liaodong Bay Depression in the Bohai Bay basin and Their Spatial Stratigraphic Distribution. Sediment. Geology.342, 78–90. 10.1016/J.sedgeo.2016.06.014
69
LiuS.GurnisM.MaP.ZhangB. (2017). Reconstruction of Northeast Asian Deformation Integrated with Western Pacific Plate Subduction since 200 Ma. Earth-Science Rev.175, 114–142. 10.1016/j.earscirev.2017.10.012
70
LiuS.LiZ.ZhangJ. F. (2004). Mesozoic basin Evolution and Tectonic Mechanism in Yanshan, China. Sci. China Ser. D47, 24–31. 10.1360/04zd0022
71
LiuS.LinC.LiuX.ZhuangQ. (2018). Syn-tectonic Sedimentation and its Linkage to Fold-Thrusting in the Region of Zhangjiakou, North Hebei, China. Sci. China Earth Sci.61, 681–710. 10.1007/s11430-017-9175-3
72
LiuS.SuS.ZhangG. (2013). Early Mesozoic basin Development in North China: Indications of Cratonic Deformation. J. Asian Earth Sci.62, 221–236. 10.1016/j.jseaes.2012.09.011
73
LiuY. M.LiuL. J.WuZ. P. (2020). New Insight into East Asian Tectonism since the Late Mesozoic Inferred from Erratic Inversions of NW-Trending Faulting within the Bohai Bay Basin. Gondwana Res.10.1016/j.gr.2020.01.022
74
LiuY. M.WuZ. P.LiuL. F. (2019). Cenozoic Fault System and Tectonic Framework of Chengbei Sag and its Adjacent Areas, Bohai Bay Basin[J]. Geotectonica et Metallogenia43 (6), 1133–1143.
75
LiuY. M.WuZ. P.LiuL. J. (2021). Cenozoic Structure and Tectonics of the Northern Beibu Gulf basin, Northern South China Sea. Tectonophysics812, 228912. 10.1016/j.gr.2020.01.022
76
LvH. B.ZhangY. X.XiaB. (2003). Syn-sedimentary Compression Structures in the Middle Triassic Flysch of the Nanpan Jiang Basin,SW China. Geol. Rev.49 (5), 449–456. (in Chinese). 10.1016/S0955-2219(02)00073-0
77
MengQ. R. (2003). What Drove Late Mesozoic Extension of the Northern China-Mongolia Tract. Tectonophysics369 (3-4), 155–174. 10.1016/s0040-1951(03)00195-1
78
MengQ.-R.WeiH.-H.WuG.-L.DuanL. (2014). Early Mesozoic Tectonic Settings of the Northern North China Craton. Tectonophysics611, 155–166. 10.1016/j.tecto.2013.11.015
79
MenziesM. A.XuY. (1998). Geodynamics of the North China Craton. Mantle Dyn. Plate Interactions East Asia27, 155–165. 10.1029/gd027p0155
80
PengJ. S.WeiA. J.SunZ. (2018). Sinistral Strike Slip of the Zhangjiakou-Penglai Fault and its Control on Hydrocarbon Accumulation in the Northeast of Shaleitian Bulge, Bohai Bay Basin, East China. Pet. Exploration Dev.45 (02), 27–38. 10.1016/s1876-3804(18)30025-9
81
QiJ. F.YangQ.LuK. Z. (2004). Geologic Map of Sub-outcrop and its Implied Information of Tectogenesis in Bohai Bay basin Province. Earth Sci. Front.11, 299–307. (in Chinese). 10.1007/BF02873097
82
QiJ. F.ZhouX. H.WangQ. S. (2010). Structural Model and Cenozoic Kinematics of Tan-Lu Deep Fracture Zone in Bohai Sea Area[J]. Geology. China37 (5), 1231–1242.
83
QiJ. F. (2004). Two Tectonic Systems in the Cenozoic Bohai Bay basin and Their Genetic Interpretation. Chin. Geology.31 (1), 15–22. (in Chinese).
84
QiJ.YangQ. (2010). Cenozoic Structural Deformation and Dynamic Processes of the Bohai Bay basin Province, China. Mar. Pet. Geology.27 (4), 757–771. 10.1016/j.marpetgeo.2009.08.012
85
QiJ.ZhouX.DengR.ZhangK. (2008). Structural Characteristics of the Tan-Lu Fault Zone in Cenozoic Basins Offshore the Bohai Sea. Sci. China Ser. D-earth Sci.51, 20–31. 10.1007/s11430-008-6013-x
86
RatschbacherL.HackerB. R.CalvertA. (2003). Tectonics of the Qinling (Central China): Tectonostratigraphy, Geochronology, and Deformation History. Tectonophysics366 (1), 1–53. 10.1016/s0040-1951(03)00053-2
87
RenJ.TamakiK.LiS.JunxiaZ. (2002). Late Mesozoic and Cenozoic Rifting and its Dynamic Setting in Eastern China and Adjacent Areas. Tectonophysics344, 175–205. 10.1016/s0040-1951(01)00271-2
88
SantoshM.ZhaoD.KuskyT. (2010). Mantle Dynamics of the Paleoproterozoic North China Craton: A Perspective Based on Seismic Tomography. J. Geodynamics49 (1), 39–53. 10.1016/j.jog.2009.09.043
89
ShanY.GongF.LinG.WangY.YanD.-P.ZhouM.-F.et al (2006). Discussion on Mesozoic Extensional Structures of the Fangshan Tectonic Dome and Their Subsequent Reworking during Collisional Accretion of the North China BlockJournal, Vol. 163, 2006, 127-142. J. Geol. Soc.163 (6), 1051–1055. 10.1144/0016-76492006-026
90
SunY. H.QiJ. F.LvY. F. (2008). Characteristics of Fault Structure and its Control to Hydrocarbon in Bozhong Depression. Acta Petrolei Sinica29 (05), 669–675. (in Chinese). 10.3321/j.issn:0253-2697.2008.05.007
91
SuoY. H.LiS. Z.LiuX. (2013). Structural Characteristics of NWW-Directed Active Fault Zones in East China: A Case Study of the Zhangjiakou-Penglai Fault Zone. Acta Petrologica Sinica29 (03), 953–966. (in Chinese). CNKI:SUN:YSXB. 10.2013-03-018.
92
TengC.HaoF.ZouH.ZhouX.XuC. (2016). Tan-Lu Fault System and its Significance in Oil Accumulation in the central Liaodong Bay Subbasin, Bohai Bay Basin, China. Bulletin100 (02), 289–314. 10.1306/10221515011
93
TianF. H.JiangZ. X. (2008). Promotion of Strata Uplift and Erosion to Hydrocarbon Accumulation. J. Southwest Pet. Univ. (Science Tech. Edition)30 (5), 37–40+13. (in Chinese). 10.3863/j.issn.1000-2634.2008.05.008
94
TongH. M.ZhaoB. Y.CaoZ. (2013). Structural Analysis of Faulting System Origin in the Nanpu Sag, Bohai Bay BasinCNKI:SUN:DZXE. Acta Geologica Sinica87 (11), 1647–1661. (in Chinese). 0.2013-11-002.
95
TongJ.ChuD.LiangL.ShuW.SongH.SongT.et al (2019). Triassic Integrative Stratigraphy and Timescale of China. Sci. China Earth Sci.62 (1), 189–222. 10.1007/s11430-018-9278-0
96
TongK.ZhaoC.LüZ.ZhangY.ZhengH.XuS.et al (2012). Reservoir Evaluation and Fracture Chracterization of the Metamorphic Buried hill Reservoir in Bohai Bay Basin. Pet. Exploration Dev.39, 62–69. 10.1016/S1876-3804(12)60015-9
97
WanG. M.TangL. J.ZhouX. H. (2009). Tectonic Characteristics of the Tanlu Fault Zone in Bodong Area of Bohai Sea. ACTA PETROLEI SINICA30 (03), 342–346. (in Chinese). 10.3321/j.issn:0253-2697.2009.03.004
98
WangG.MitchellT. M.MeredithP. G.NaraY.WuZ. (2016). Influence of Gouge Thickness and Grain Size on Permeability of Macrofractured basalt. J. Geophys. Res. Solid Earth121 (12), 8472–8487. 10.1002/2016jb013363
99
WangQ.ZouH.HaoF.ZhuY.ZhouX.WangY.et al (2014). Modeling Hydrocarbon Generation from the Paleogene Source Rocks in Liaodong Bay, Bohai Sea: A Study on Gas Potential of Oil-Prone Source Rocks. Org. Geochem.76, 204–219. 10.1016/j.orggeochem.2014.08.007
100
WangR. B.GuG. H.XuJ. (2005). Discussion on Characteristics of Crustal Deformation along the Zhangjiakoubohai Seismotectonic Zone. Earthquake Res. China19 (03), 327–337. (in Chinese). 10.1007/BF02873097
101
WangT.ZhengY.ZhangJ.ZengL.DonskayaT.GuoL.et al (2011). Pattern and Kinematic Polarity of Late Mesozoic Extension in continental NE Asia: Perspectives from Metamorphic Core Complexes. Tectonics30 (6), a–n. 10.1029/2011TC002896
102
WangY.SunL.ZhouL.XieY. (2018a). Discussion on the Relationship between the Yanshanian Movement and Cratonic Destruction in North China. Sci. China Earth Sci.61 (5), 499–514. 10.1007/s11430-017-9177-2
103
WangY.ZhouL.LiuS.LiJ.YangT. (2018b). Post-cratonization Deformation Processes and Tectonic Evolution of the North China Craton. Earth-Science Rev.177, 320–365. 10.1016/j.earscirev.2017.11.017
104
WangZ.-c.DengQ.-d.DuX.-s.ChaoH.-t.WuZ.-q.XiaoL.-x.et al (2006). Active Fault Survey on the Tanlu Fault Zone in Laizhou Bay. Acta Seimol. Sin.19 (5), 530–541. 10.1007/s11589-006-0506-5
105
WuF.XuY.ZhuR.ZhangG. (2014). Thinning and Destruction of the Cratonic Lithosphere: A Global Perspective. Sci. China Earth Sci.57 (12), 2878–2890. 10.1007/s11430-014-4995-0
106
WuZ. P.HouX. B.LiW. (2007). Discussion on Mesozoic Basin Patterns and Evolution in the Eastern North China Block. Geotectonica et Metallogenia31 (04), 385–399. (in Chinese). 10.3969/j.issn.1001-1552.2007.04.001
107
WuZ. P.ZhangF. P.LiW. (2020). Apatite Fission Track Evidence of Mesozoic Tectonic Evolution in the Huanghua Depression. J. China Univ. Mining Tech.49 (01), 123–136. (in Chinese).
108
WuZ. P.ZhangJ.RenJ. (2016). Development Characteristic of Strike-Slip Duplex in the Eastern Part of Liaodong Bay Depression and its Petroleum Geological Significance. Acta Geologica Sinica90 (05), 848–856. (in Chinese). 10.3969/j.issn.0001-5717.2016.05.002
109
WuZ.ChengY.YanS.SuW.WangX.XuC.et al (2013). Development Characteristics of the Fault System and its Control on basin Structure, Bodong Sag, East China. Pet. Sci.10 (04), 450–457. 10.1007/s12182-013-0295-0
110
XiD.WanX.LiG.LiG. (2019). Cretaceous Integrative Stratigraphy and Timescale of China. Sci. China Earth Sci.62 (1), 256–286. 10.1007/s11430-017-9262-y
111
XuC. G.RenJ. Y.WuZ. P. (2015). Cenozoic Fault System and Tectonic Evolution of the Eastern Liaodong Bay Depression. Geol. J. China Universities21 (2), 215–222. (in Chinese). 10.16108/j.issn1006-7493.2014170
112
XuC. G. (2016). Strike-Slip Transfer Zone and its Control on Formation of Medium and Large-Sized Oilfields in Bohai Sea Area. Editorial Committee Earth Science-Journal China Univ. Geosciences41 (09), 1548–1560. 10.3799/dqkx.2016.508
113
XuC.YuH.WangJ.LiuX. (2019). Formation Conditions and Accumulation Characteristics of Bozhong 19-6 Large Condensate Gas Field in Offshore Bohai Bay Basin. Pet. Exploration Dev.46, 27–40. (in Chinese). 10.11698/PED.2019.01.0310.1016/s1876-3804(19)30003-5
114
XuG.ZhaoY.GaoR. (2006). Mesozoic Basin Deformation of Yanshan Folded Fault Belt — Records of the Intraplate Deformation Process : A Case Study of Xiabancheng , Chengde — Shangbancheng and Beitai Basins. Acta Geoscientia Sinica27 (1), 1. 10.1007/s11442-006-0415-5
115
XuG.MaR.GongD.ZhouD.LiJ.GuoY.et al (2011). Features of the Fault System and its Relationship with Migration and Accumulation of Hydrocarbon in Liaodong Bay. Pet. Sci.8 (03), 251–263. 10.1007/s12182-011-0142-0
116
XuH.LiuY. Q. (2017). Jurassic–Cretaceous Transition Terrestrial Red Beds in Northern North China and Their Regional Paleogeography, Paleoecology, and Tectonic Evolution. Acta Geoscientia Sinica38 (z1), 25–28. (in Chinese). 10.3975/cagsb.2017.s1.08
117
XuJ.ZhouB. G.JiF. J. (2012). Features of Seismogenic Structures of Great Earthquakes in the Bohai Bay Basin Area,North China. Seismology Geology.34 (004), 618–636. (in Chinese). 10.3969/j.issn.0253-4967.2012.04.008
118
YanD.-P.ZhouM.-F.SongH.-L.WangG.-H.SunM. (2006). Mesozoic Extensional Structures of the Fangshan Tectonic Dome and Their Subsequent Reworking during Collisional Accretion of the North China Block. J. Geol. Soc.163 (1), 127–142. 10.1144/0016-764904-154
119
YangJ.-H.WuF.-Y.WildeS. A.BelousovaE.GriffinW. L. (2008). Mesozoic Decratonization of the North China Block. Geol36 (6), 467–470. 10.1130/G24518A.1
120
YangJ.WuF.ShaoJ.WildeS.XieL.LiuX. (2006). Constraints on the Timing of Uplift of the Yanshan Fold and Thrust Belt, North China. Earth Planet. Sci. Lett.246 (3-4), 336–352. 10.1016/j.epsl.2006.04.029
121
YangW. C. (2003). Flat Mantle Reflectors in Eastern China: Possible Evidence of Lithospheric Thinning. Tectonophysics369 (3), 219–230. 10.1016/S0040-1951(03)00215-4
122
YingJ.ZhangH.KitaN.MorishitaY.ShimodaG. (2006). Nature and Evolution of Late Cretaceous Lithospheric Mantle beneath the Eastern North China Craton: Constraints from Petrology and Geochemistry of Peridotitic Xenoliths from Jünan, Shandong Province, China. Earth Planet. Sci. Lett.244 (3-4), 622–638. 10.1016/j.epsl.2006.02.023
123
ZhaiM. G.LiuW. J. (2003). Palaeoproterozoic Tectonic History of the North China Craton: a Review. Precambrian Res.122 (1-4), 183–199. 10.1016/s0301-9268(02)00211-5
124
ZhaiM.FanQ.ZhangH.SuiJ.ShaoJ. a. (2007). Lower Crustal Processes Leading to Mesozoic Lithospheric Thinning beneath Eastern North China: Underplating, Replacement and Delamination. Lithos96 (1-2), 36–54. 10.1016/j.lithos.2006.09.016
125
ZhanR.ZhuG.YangG. L. (2013). The Genesis of the Faults and the Geodynamic Environment during Neogene for Offshore of the Bohai Sea. Earth Sci. Front.20 (4), 151–165. (in Chinese).
126
ZhangB.ZhuG.ChenY.PiaoX.JuL.WangH. (2012). Deformation Characteristics and Genesis of the Waziyu Metamorphic Core Complex in Western Liaoning of China. Sci. China Earth Sci.55 (011), 1764–1781. 10.1007/s11430-012-4495-z
127
ZhangC. H.SongH. L.WangG. H. (2001). Mesozoic Dextral Strike-Slip Structural System in Middle Segment of Intraplate Yanshan Orogenic belt, Northern China. J. China Univ. Geosciences26 (05), 464–472. (in Chinese). 10.3321/j.issn:1000-2383.2001.05.004
128
ZhangC. H.ZhangY.LiH. L. (2006). Late Mesozoic Thrust Tectonics Framework in the Western Part of the Yanshan Orogenic belt and the Western Hills of Beijing:characteristics and Significance. Earth Sci. Front.02, 165–183. (in Chinese). 10.3321/j.issn:1005-2321.2006.02.015
129
ZhangC.LiC.DengH.LiuY.LiuL.WeiB.et al (2011). Mesozoic Contraction Deformation in the Yanshan and Northern Taihang Mountains and its Implications to the Destruction of the North China Craton. Sci. China Earth Sci.54 (6), 798–822. 10.1007/s11430-011-4180-7
130
ZhangJ.LiW.WuZ. P. (2017). Structural Characteristics of Tan-Lu Fault Zone in South Area of Bohai Sea and its Control on Basin Structure[J]. Earth Sci.42 (9), 1549–1564.
131
ZhangQ.WangY. L.JinW. J. (2008). Eastern China Plateau during the Late Mesozoic: Evidence, Problems and Implication. Geol. Bull. China27 (9), 1404–1430.
132
ZhangX. Q.WuZ. P.ZhouX. H. (2017). Cenozoic Tectonic Characteristics and Evolution of the Southern Bohai Sea. Geotectonica et Metallogenia41 (1), 50–60. 10.16539/j.ddgzyckx.2017.01.004
133
ZhangY. Q.DongS. W.ZhaoY. (2007). Jurassic Tectonics of North China: a Synthetic View. Acta Geologica Sinica81 (11), 1462–1480. (in Chinese). 10.3321/j.issn:0001-5717.2007.11.002
134
ZhaoG. (2001). Palaeoproterozoic Assembly of the North China Craton. Geol. Mag.138 (1), 87–91. 10.1017/S0016756801005040
135
ZhaoX.JinF.WangQ.BaiG. (2015). Buried-hill Play, Jizhong Subbasin, Bohai Bay basin: A Review and Future Propespectivity. Bulletin99 (01), 1–26. 10.1306/07171413176
136
ZhaoY.XuG.ZhangS. H. (2004). Yanshanian Movement and Conversion of Tectonic Regimes in East Asia. Earth Sci. Front.11 (3), 319–328. (in Chinese)10.3321/j.issn:1005-2321.2004.03.030
137
ZhouL. H.LiS. Z.LiuJ. Z. (2003). The Yanshanian Structural Style and basin Prototypes of the Mesozoic Bohai Bay Basin. Prog. Geophys.18 (4), 692–699. (in Chinese). 10.3969/j.issn.1004-2903.2003.04.019
138
ZhuG.LiuG. S.NiuM. L. (2003). Transcurrent Movement and Genesis of the Tan-Lu Fault Zone. Geol. Bull. China22, 200–207. 10.1016/S0955-2219(02)00073-0
139
ZhuG.ChenY.JiangD.LinS. (2015). Rapid Change from Compression to Extension in the North China Craton during the Early Cretaceous: Evidence from the Yunmengshan Metamorphic Core Complex. Tectonophysics656, 91–110. 10.3969/10.1016/j.tecto.2015.06.009
140
ZhuG.LiuG. S.NiuM. L.XieC. L.WangY. S.XiangB. (2009). Syn-collisional Transform Faulting of the Tan-Lu Fault Zone, East China. Int. J. Earth Sci. (Geol Rundsch)98 (1), 135–155. 10.1007/s00531-007-0225-8
141
ZhuG.WangY.LiuG.NiuM.XieC.LiC. (2005). 40Ar/39Ar Dating of Strike-Slip Motion on the Tan-Lu Fault Zone, East China. J. Struct. Geology.27 (8), 1379–1398. 10.1016/j.jsg.2005.04.007
142
ZhuJ. C.FengY. L.MengQ. R. (2020). Late Mesozoic Tectonostratigraphic Division and Correlation of Bohai Bay basin:Implications for the Yanshanian Orogeny. Yanshanian Orogeny50 (01), 28–49.
143
ZhuR.ChenL.WuF.LiuJ. (2011). Timing, Scale and Mechanism of the Destruction of the North China Craton. Sci. China Earth Sci.54 (006), 789–797. 10.1007/s11430-011-4203-4
144
ZhuY.LiuS.ZhangB.GurnisM.MaP. (2021). Reconstruction of the Cenozoic Deformation of the Bohai Bay Basin, North China. Basin Res.33 (1), 364–381. 10.1111/bre.12470
145
ZuoY.QiuN.ZhangY.LiC.LiJ.GuoY.et al (2011). Geothermal Regime and Hydrocarbon Kitchen Evolution of the Offshore Bohai Bay Basin, North China. Bulletin95 (5), 749–769. 10.1306/09271010079
Summary
Keywords
WNW-directed faults, development characteristics, evolution process, formation mechanism, Liaodong Bay subbasin
Citation
Li W, Meng M, Zhang T, Chen X, Liu Y, Wang D, Yang H and Niu C (2022) New Insights into the Distribution and Evolution of WNW-Directed Faults in the Liaodong Bay Subbasin of the Bohai Bay Basin, Eastern China. Front. Earth Sci. 9:763050. doi: 10.3389/feart.2021.763050
Received
23 August 2021
Accepted
17 December 2021
Published
02 March 2022
Volume
9 - 2021
Edited by
Xunhua Zhang, Qingdao Institute of Marine Geology (QIMG), China
Reviewed by
Wang Jun, Chengdu University of Technology, China
Chengchuan Gu, Anhui University of Science and Technology, China
Updates
Copyright
© 2022 Li, Meng, Zhang, Chen, Liu, Wang, Yang and Niu.
This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Tongjie Zhang, zhangtj13@cnooc.com.cn
This article was submitted to Structural Geology and Tectonics, a section of the journal Frontiers in Earth Science
Disclaimer
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article or claim that may be made by its manufacturer is not guaranteed or endorsed by the publisher.