Structural deformation and its implication for hydrocarbon accumulation in the Wuxia fault belt, northwestern Junggar basin, China

Shuai Sun; Sen Yang; Wenjun He; Menglin Zheng; Yang Zou; Liliang Huang; Yi Zhao; Wei Song

doi:10.1515/geo-2022-0452

Article Open Access

Structural deformation and its implication for hydrocarbon accumulation in the Wuxia fault belt, northwestern Junggar basin, China

Shuai Sun , Sen Yang , Wenjun He , Menglin Zheng , Yang Zou , Liliang Huang , Yi Zhao and Wei Song

Published/Copyright: February 13, 2023

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From the journal Open Geosciences Volume 15 Issue 1

Abstract

With the great discovery of unconventional oil in the Fengcheng Formation in the Mahu sag, the Wuxia fault belt, which shows similar lithological characteristics and lithofacies, is considered the most favorable area for future petroleum exploration. However, the complicated structural patterns remain unclear and restrict the petroleum exploration and development. In this study, combined with new seismic data and some borehole data, we conclude the structural styles in the Wuxia fault belt and analyze their distribution characteristics, and further investigate their implications for tectonic evolution and hydrocarbon accumulation. Five typical seismic sections are captured from the west to the east of the fault belt. Decollement folds and fold accommodation faults superimpose on the underlying basement fault related folds. Structure patterns also show a zonation in S–N direction and a segmentation in E–W direction. The balanced section reveals that the present-day structure features were fundamentally formed by Late Permian. The structural deformation shows distinctive features of a foreland basin which may develop in Early Permian and continue until the Late Permian. The oil reservoirs in the Fengcheng Formation in deeper detachment fold and the autochthonous Fengcheng Formation in fault propagation folds are the most favorable regions for further unconventional petroleum exploration.

Keywords: structure style; hydrocarbon accumulation; Fengcheng Formation; Wuxia fault belt; Junggar basin; foreland basin

1 Introduction

With the increasing demands of oil and gas around the world, unconventional hydrocarbon resources show more and more importance in petroleum exploration and development. Shale oil, shale gas, tight oil and other unconventional resources gradually become the research hotspots, and an increasing number of unconventional oil fields have been discovered in recent years. In Junggar basin, northwestern China, Permian Fengcheng Formation in the Mahu sag is considered the most potential field for shale oil exploration, since Permian Lucaogou Formation in the Jimusar sag is estimated with quantities of 14.3 billion tons’ oil and 7,868 billion m³ gas [1,2,3,4]. As continuous exploration wells are drilled in the Mahu sag, researchers and engineers found that conventional oil reservoirs, tight oil and shale oil orderly coexist in the Fengcheng Formation and gradually change from the northeast to the southwest (Figure 1) [5]. In the Wuxia fault belt, the Fengcheng Formation shows lithologic characteristics and lithofacies similar to that in the Mahu sag, which means shale oil and tight oil may also be largely accumulated in this fault belt. This makes the Wuxia fault belt the most favorable area for future exploration of unconventional petroleum.

Figure 1

(a) Simplified map of China and location of the Junggar basin and (b) orderly coexistence model of conventional and unconventional hydrocarbons in Fengcheng Formation in the Mahu sag (modified after Zhi et al. [5]).

The Wuxia fault belt is a foreland thrust belt under the orogenic movement during the Late Hercynian time, and has undergone multiphase deformation histories at a later stage [6,7,8,9,10]. Faults are widely developed in this fault belt, causing the complicated structures. Therefore, studying the structural deformation and its implication for hydrocarbon accumulation in the Wuxia fault belt is extremely important for further petroleum exploration. Previous literatures investigated the structural deformation of the Wuxia fault belt [11,12,13,14,15], but few researchers consider the entire fault belt to investigate the structural deformation. Some focused only on structural deformation in the Mt. Halaalate area or the leading edge of the fault belt. This is due to the different ownership of mineral rights and lacking of enough seismic data. Besides, lacking of drilling data constrained the strata and previous seismic data with poor quality severely restricted the structural deformation analysis. In recent years, new high-resolution three-dimensional seismic data covering the southern region of the fault belt is available. Combined with the seismic data covering the northern region of the fault belt which is obtained from Sinopec and some 2D profiles, it provides sufficient conditions for investigating the structural deformation of the Wuxia fault belt. In this study, based on seismic data and drilling data, we conclude the structural styles in the Wuxia fault belt and analyze their distribution characteristics, and further investigate their implication for hydrocarbon accumulation.

2 Geological setting

The Junggar basin is located in the northwest part of China, covering an area of about 130,000 km² (Figure 1). It is an important tectonic component of the Central Asian Orogenic Belt, located in the conjunction area of Siberian craton, Russian craton and Tarim craton (Figure 2) [16,17]. The basin is a superimposed basin developed from the Late Paleozoic to Cenozoic [18,19,20,21]. The Wuxia fault belt is located in the northern margin of the Junggar basin. It covers an area of 1,000 km² with a length of 80 km and a width of 16 km (Figure 2). The Wuxia fault belt lies in the eastern part of the foreland thrust belt and bounded by the Kebai fault belt to the west, the Mahu sag to the south and the Yaxian uplift to the southeast. In the period of Late Carboniferous to Early Permian, the Wuxia fault belt was formed by the collision between the Kazakhstan plate and ancient Junggar block [22,23]. Since the Late Permian, the fault belt was superimposed multiphase tectonic deformation, causing the sediments to undergo strong uplift and severe erosion [8,12,23,24].

Figure 2

Sketch maps showing the (a) tectonic location of the Junggar basin (modified after Xu et al. [16]) and (b) tectonic units of the western Junggar basin (modified after Wang et al. [21]) and location of the selected five seismic sections AA′ to EE′ from west to east.

The Wuxia fault contains a Carboniferous to Cenozoic sedimentary succession, including the Permian Jiamuhe Formation, the Fengcheng Formation, the Xiazijie Formation, the Lower Wuerhe Formation and Triassic Baikouquan Formation, Karamay Formation and Baijiantan Formation (Figure 3) [19,25]. The Carboniferous strata are dominated by volcanic rocks, pyroclastic rocks, conglomerates, sandstones and mudstones [7,8]. The Jiamuhe Formation consists of volcanic rocks, conglomerates, sandstones and mudstones [8,26]. The Fengcheng Formation is composed of dolomitic shales, dolomitic siltstones and sandstones with alkaline minerals or evaporates, with thickness up to 1,700 m [27,28]. From the Carboniferous to the Early Permian, the general depositional background changed from shallow marine environment to semi-closed shallow alkaline lake environment [18,29,30]. The Fengcheng Formation can be subdivided into three members, the upper and middle members (P₁f_2–3) are characterized by fine grained sediments and the lower member (P₁f₁) consists of pyroclastic sediments and mudstones [5,31,32]. It is mainly the most important source rocks in the fault belt and adjacent to Mahu sag [33,34]. In the fault belt, several oil-bearing formations have been found, including the Permian Fengcheng, the Triassic Baikouquan, Karamay, the Jurassic Badaowan and Xishanyao Formations (Figure 3) [35,36,37].

Figure 3

Comprehensive tectono-stratigraphic columns of the Junggar basin. The Fengcheng Formation is the main source rock in the western Junggar basin and the favorable layer for unconventional exploration.

3 Structural deformation analysis

3.1 Structural patterns

Structural styles refer to the general characteristics of structures closely related to shapes, distribution and mechanism, showing the general characteristics of structural deformation [38,39,40,41]. Based on seismic interpretation, strata, faults and their combinations are identified, and the structural styles and structural deformation are further analyzed. Here five typical seismic profiles are captured from the west to the east of the Wuxia fault belt (Figure 4).

Figure 4

Seismic profiles of typical structural styles in the Wuxia fault belt. (a) Profile a is the section AA′, (b) profile b is the section BB′, (c) profile c is the section CC′, (d) profile d is the section DD′, and (e) profile e is the section EE′ (see section location in Figure 2).

Profile A-A′ lies in the west of the fault belt, the structures are dominated by compressional structures, including several fault-related folds and a buckle fold in the southern area (Figure 4a). The faulted folds can be further subdivided into several fault-propagation folds, a back thrust structure. In piedmont region, the fault-propagation fold, bounded by two basement faults F1 and F2 with N-S inclination, is characterized by large fault displacement and the strata are highly uplifted and denudated. In the southern area of the fault belt, a fault-propagation fold with little displacement is developed in deep layers and a buckle fold is formed in shallow layers (T-P₁f).

From the profile B-B′, the structures consist of strike-slip structures and compressional structures (Figure 4b). A positive flower structure develops in the northern part of the fault belt, consisting of a strike slip fault with high angle and several basement reverse faults developed from bottom to top. Compressional structures are made up of some fault-related folds and a decollement fold, and the faulted folds are made up of several fault-propagation folds, a back thrust structure and an imbricate faulted fold. A fault-propagation fold with large displacement and height of uplift develops in piedmont region (Figure 4b). A decollement fault develops in the Fengcheng Formation and a decollement fold is formed in the middle fault belt. Noticeably, in the deep layers, several fault-propagation folds develop beneath the decollement fold and the fault-propagation fold to the north of fault F2 (Figure 4b). A back thrust structure develops at the frontal part of the fault belt. The decollement fold and the fault-propagation fold in shallow layers are largely thrusted above these fault-propagation folds in deep layers with large horizontal displacement.

Profile C-C′ lies in the middle of the fault belt, the main structures are strike-slip structures and compressional structures (Figure 4c). Similar to profile B-B′, in the northern part of the fault belt, a strike slip fault and several basement reverse faults give the belt an overall appearance of a positive flower structure. A decollement fault (F2) develops in the Fengcheng Formation and a north-dipping monocline appears in piedmont region. At the leading edge of the monocline, a decollement fold developments and the Fengcheng formation gets thicker at the core of decollement fold (Figure 4c). At the south limb of the decollement fold, a reverse fault (F3) develops which is assumed as a fold-accommodation fault structure. Moreover, in adjacent areas, two types of forelimb space accommodation thrusts and forelimb shear thrusts are formed where the reverse faults in the decollement fold are assumed as passive faults as a result of variation in fold deformation (Figure 5). At the frontal fault belt, two north-dipping reverse faults (F4-1 and F4-2) develop and merge into a decollement fault that formed in the Fengcheng Formation. Besides, back thrust structures and triangle zones exist in the Triassic to middle Permian strata, and these structures show shallow level and autochthonous thrusting features. At deeper depth beneath the autochthonous compressional structures, three basement reverse faults distribute in the middle Permian to Carboniferous strata and merge into a main thrusting fault (F5), which show the appearance of imbricate thrust structure (Figure 4c). Similar to other profiles, a back thrust structure is formed at the front of the fault belt. The monocline and the decollement fold in the Permian are thrusted largely superimposing on the fault-propagation fold in deeper depth.

Figure 5

Summarized classification of structural styles in the Wuxia fault belt. Structures are divided into four types of structure styles, including fault-related fold, fold accommodation fault, fold and flower structure. (a) Fault propagation fold, a kind of fault-related fold. (b) Back thrust structure, a kind of fault-related fold. (c) Triangle zone, a kind of fault-related fold. (d) Imbricate thrust structures, a kind of fault-related fold. (e) Forelimb shear thrust, a kind of fold accommodation fault. (f) Forelimb space accommodation thrust, a kind of fold accommodation fault. (g) Buckle fold, a kind of fold. (h) Decollement fold, a kind of fold. (i) Positive flower structure, a kind of flower structure. The locations of typical seismic structure sections are shown in Figure 6.

In the east of the fault belt, several 2D seismic profiles are only available (Figure 4d and e). From profile D-D′, the structure patterns are similar to the patterns of profile C-C′, including the positive flower structure. In piedmont region, a decollement fault (F2) with great uplift and large horizontal displacement develops in the Fengcheng Formation and a decollement fold is formed which can be simplified as a monocline (Figure 4d). To the south, two sets of autochthonous fault-propagation folds are formed in the shallow strata (T-P1f) and deeper layers (P-C), respectively. One diffidence is that no decollement fold develops at the leading edge of the monocline, the second is that fewer back thrust structures are formed at the frontal fault belt. From profile E-E′, fault-propagation folds are widely distributed and show an overall feature of imbricate faulted folds (Figure 4e).

Generally, structures in the Wuxia fault belt can be classified into compressional structures and strike-slip structures (Figure 5). The compressional structures can be subdivided into fault-related folds, folds and fold-accommodation faults. Fault propagation folds, back thrust structures, triangle zones and imbricate thrust structures are widely distributed in the Wuxia fault belt. Folds in the fault belt are mainly buckle folds and decollement folds. Besides, two types of fold accommodation faults including forelimb space accommodation thrusts and forelimb shear thrusts develop in the fault belt. The strike-slip structure formed in the fault belt is positive flower structure.

3.2 Vertical and planar distribution

On the basis of the typical structure styles identified in seismic sections, vertical and planar distribution characteristics are summarized in this study. In the vertical direction, it can be found that structure styles show obvious differences in shallow and deeper depth (Figure 4). Structures in shallow depth are characterized by thrust nappe with large lateral displacement and uplift. Decollement folds and fold accommodation faults related to decollement folds above Fengcheng Formation decollement fault exist in shallow depth. Structures in deeper depth under the decollement fault are dominated by fault propagation fold in lower Permian–Carboniferous layers and generally show an appearance of imbricate structures.

Moreover, structures have a regular distribution in plane, and mainly show a zonation in S–N direction and a segmentation in E–W direction (Figures 4 and 6). In the middle part of the fault belt, a decollement fault with large horizontal displacement develops in the Fengcheng Formation such that a decollement fold develops in the upper Permian layers. In piedmont region, a fault propagation fold develops to the north of the decollement fold which possibly experienced more intense deformation than the other regions. To the south, fault related folds develop in the Triassic–Permian layers, and back thrust structures are formed at the leading edge of the fault belt.

Figure 6

Planar distribution of structural styles in the Wuxia fault belt. Note: the black circles represent structural styles of structures in shallow depth, and the orange cycles represent structures underlying the shallow structures at the frontal fault belt.

In the eastern fault belt, the region exhibited weak deformation with weak decollement, and no obvious thrust nappe exists (Figures 4 and 6). The middle-eastern part experienced intense deformation which is featured by decollement folding. The middle part also underwent intense deformation where decollement folding and thrusting both exist. In this region, decollement fold, fold accommodation faults and fault-related folds including back thrust structures and triangle zones are all widely developed (Figures 4 and 6). In the middle-western part, the deformation is also mainly controlled by decollement folding and thrusting, but the difference is that intense thrusting with large vertical displacement contributes to the formation of a fault-related fold to the north of the decollement fold. Besides, fold accommodation faults are less developed than that of the middle part (Figure 6). The western fault belt experienced weak deformation, no obvious decollement and thrust nappe exists.

3.3 Deformation recovery analysis

Balancing and restoration of seismic sections is conducted by stripping off each layer and restoring faults and folds. We restored one length-balanced section across the fault belt in Figure 7 with 3D Move software in this study (section BB′, see section location in Figure 2). In Early Permian (P1f), several basement faults were active and some fault-related folds developed in the Carboniferous–Permian Fengcheng Formation. In the middle Permian (P2x-P2w), the fault belt experienced intense deformation with high shortening rate, 38% in the P2x period and 17% in the P2w period. Basement faults were still active and extended upward to middle Permian strata. In this period, the fault propagation fold in piedmont region was highly uplifted, and a decollement fault developed in the Fengcheng Formation in the P2x period. In the Late Permian, the fault belt was still in a compressional field and experienced a deformation with a shortening rate of 22%. The decollement fault extended upward and a decollement fold developed in the Permian strata. In this period, the decollement fold and the fault propagation fold to the north were highly uplifted and underwent intense denudation to create an erosional angular unconformity at the base of the Triassic, meanwhile back thrust structure was formed at the leading edge of the fault belt. Up to the Late Permian, the present-day structure features of the fault belt were fundamentally formed where a decollement fold above Fengcheng Formation superimposed on the underlying basement fault-related folds. The balanced section shows that the Triassic–Cretaceous sequences overlap the fault belt and no intense thrusting activities existed during that time. However, from seismic sections in the middle part of the fault belt (Figure 4c), it can be found that local thrusting and uplifting movement developed, the faults in the fault belt reactivated but the structural pattern remains relatively stable. The basement faults and decollement fault have been active for several times in the Jurassic and Cretaceous to cut unconformities at the base of the Jurassic and Cretaceous (Figure 4). However, they did not contribute significantly to the formation of the Wuxia fault belt.

Figure 7

A length-balanced section from Well HS2 to Well FN4 constructed in the Wuxia fault belt (see location and orientation of the section in Figure 2).

4 Discussion and implications

4.1 Tectonic evolution of northwestern Junggar basin

The tectonic setting of northwestern Junggar basin since Late Carboniferous remains a controversial issue. However, in recent years, researchers tend to accept that the northwestern margin of Junggar basin was in a subduction-related tectonic setting in the Late Carboniferous [8,42,43]. At the end of Late Carboniferous, the western Junggar orogenic belt was formed by the collision between the Junggar plate and the Kazakhstan plate [44,45,46]. However, the tectonic setting of northwestern Junggar basin in the Permian still remains a hot debate, especially in the Early Permian. In the Early Permian (P1j and P1f), some researchers proposed that the northwestern Junggar basin experienced a tectonic transition from the subduction in Late Carboniferous to the foreland basin [17,18,24,42,47]. Some researchers argue that the western Junggar basin entered the post-collisional extension stage by analyzing the geochemical characteristics of magmas [8,45], and some geoscientists propose that a rift basin developed in the northwestern margin by analyzing soft-sediment deformation structures in the Fengcheng Formation [3,48]. According to our research, the structural deformation in the Wuxia fault belt owns distinctive features of a foreland basin (Figures 4 and 5). Besides, when the Early Permian Fengcheng Formation was deposited, several reverse faults developed and thrusting activities continued until the end of the Permian, during which several strong activities occurred (Figure 7). This suggests that the collision between the Kazakhstan plate and the Junggar plate remained active until the Late Permian. Moreover, in the Wuxia fault belt, the development of detachment folds and fold accommodation faults verify that the extremely thick mudstones of Fengcheng Formation lay the rock material foundation for long-distance thrusting and detachment, and this may be the reason why soft deformation in a foreland basin develops in the Fengcheng Formation.

4.2 Implications for hydrocarbon accumulation

Permian Fengcheng Formation is considered the main source rock in the Mahu sag and adjacent areas. Intense faulting and folding in the fault belt has changed the original distribution of the source rocks. Previous literature have investigated the sedimentary paleo-environment of the Early Permian strata, and the Fengcheng Formation is assumed as the product of a semi-deep to deep alkaline lake [3,8,29,49]. Feng et al. (2018) demonstrated that the Paleo-Junggar lake may have reached at least the Darbut area in the Early Permian, or even the northern Heshitologa basin. The balanced section constructed in this study also indicates that large lateral displacement and intense uplift exist in the northwestern Junggar basin, the distribution of source rocks is greatly affected and reconstructed in the Wuxia area. With the discovery of shale oil and tight oil in the Mahu sag, the Wuxia fault belt may be the potential region for further exploration of unconventional petroleum. In recent years, an exploration well FC3 was drilled at the hinge of the decollement fold, and thick dolomitic mudstones or siltstones of Fengcheng Formation with a thickness of nearly 700 m were encountered during the drilling process (Figure 8). This further proves that the Fengcheng Formation is thickened by decollement folding. Moreover, intense thrusting in the Wuxia fault belt contributes to the superimposition of Fengcheng Formation on the autochthonous source rocks (Figure 8). The thrusting also results in the uplift and denudation of Fengcheng Formation in piedmont region.

Figure 8

Schematic diagram of the distribution of unconventional oil and gas in the Fengcheng Formation in the Wuxia fault belt (see location and orientation of the section FF′ in Figure 2).

Fractures are crucial for shale oil and tight oil exploration. Faulting and folding both contribute to the development of fractures, and the fractures are mainly developed in areas near faults, the hinge and core of the fold [50,51,52,53]. In the Wuxia fault belt, fault-related folds, decollement folds and fold accommodation faults are widely developed. Due to continuous intense faulting and folding, fractures are also widely developed in the Fengcheng Formation, especially in areas near faults (Figure 8). In addition, some tensile fractures may develop at the hinge of the decollement fold, which is beneficial for improving the quality of reservoirs. Moreover, drilled wells reveal that the main storage spaces of the Fengcheng Formation are dissolved pores, residual inter-granular pores and micro-fractures. The porosity of the Fengcheng Formation in the fault belt is assumed to be larger than that of the Mahu sag.

Fengcheng Formation is matured and begins to generate hydrocarbons in the Late Permian [11,54]. At this time, hydrocarbons are accumulated in Permian strata, but are damaged by the intense uplift and denudation in the fault belt. As a result of the thrusting, the autochthonous source rocks of Fengcheng Formation underlying the decollement fault are buried rapidly and may begin to generate large amounts of hydrocarbons, and hydrocarbon generation of source rocks on the thrust belt may be stagnated. At the end of the Triassic, the source rocks of Fengcheng Formation in the Mahu sag and the source rocks of the autochthonous Fengcheng Formation underlying the decollement fault generate large amounts of hydrocarbons. Then, oil and gas migrate upward through faults and ultimately accumulate in favorable traps in the fault belt, such as X69 oil-gas reservoir, FC3 oil reservoir, HS2 oil reservoir etc. FC3 oil reservoir is characterized by dark heavy oil with a density of 0.959 g/cm³. After the Triassic, the fold accommodation faults developed near Well FC3 may all contribute to the damage of reservoir. Generally, faults developing in the thrusting activities provide a conduit for hydrocarbon migration from autochthonous source rocks to the fault belt. Besides, intense uplift and denudation caused by tectonic activities may have a destructive effect on the accumulated hydrocarbon.

In the Wuxia fault belt, oil reservoirs of the Fengcheng Formation in different structural styles are superimposed vertically, showing a tridimensional oil-bearing characteristic (Figure 8). Great discovery of unconventional petroleum has been found in the Mahu sag, and recent exploration reveals that the oil reservoirs in shallow depth may be damaged. The oil reservoirs may exist in the Fengcheng Formation in the deeper detachment fold and the autochthonous Fengcheng Formation in the fault propagation fold. These oil reservoirs are the most favorable regions for further exploration.

5 Conclusion

Based on new seismic data and drilling data, this work concludes the structural styles and their distribution characteristics, and further investigates their implication for hydrocarbon accumulation in the Wuxia fault belt, northwestern Junggar, China. Results show that the compressional structures can be subdivided into fault-related folds, folds and fold accommodation faults, and the strike-slip structure is a positive flower structure. In the vertical direction, structures in shallow depth are characterized by thrust nappe. Decollement folds and fold accommodation faults above decollement fault exist in shallow depth. Structures underlying the decollement fault are dominated by fault propagation fold in the lower Permian–Carboniferous layers and generally show an appearance of imbricate structures. Structure patterns also show a zonation in S–N direction and a segmentation in E–W direction. In the middle part, a decollement fold develops in the upper Permian layers, and to the north, a fault propagation fold develops in the lower Permian–Carboniferous. To the south, fault-related folds develop in the Triassic–Permian layers. The eastern and western fault belts experienced weak deformation, no or weak decollement and no obvious thrust nappe exists. The middle part experienced intense deformation where decollement fold, fold accommodation faults and fault-related folds are developed. We also conducted one balanced section across the fault belt. Results show that it is until the Late Permian that the present-day structure features of the fault belt were fundamentally formed. The structural deformation in the Wuxia fault belt shows distinctive features of a foreland basin which may develop in the Early Permian and continue until the Late Permian. The distribution of source rocks is reconstructed and the source rocks get thickened by decollement folding and thrusting in the Wuxia area. Fractures and dissolved pores are developed in the Fengcheng Formation which improve the quality of reservoirs. Faults developing in the thrusting activities provide a conduit for hydrocarbon migration. Meanwhile, tectonic activities may have a destructive effect on the accumulated hydrocarbon.

Acknowledgements

We thank three anonymous reviewers for their constructive comments and suggestions. This work is supported by funds from the PetroChina Science and Technology Major Project (No. 2021DJ0405, 2021DJ2205, 2022KT0302 and 2022KT0406).

Author contributions: S.S. and S.Y. interpreted the seismic profiles; S.S. and M.Z. analyzed the structural deformation; W.H. and Y.Z. analyzed the implications for hydrocarbon; L.H. and Y.Z. constructed the balanced sections; S.S. prepared the original manuscript; W.S. and S.S. reviewed and revised the manuscript; The authors applied the SDC approach for the sequence of authors.
Conflict of interest: The authors declare no conflict of interest.
Data availability statement: The data supporting the findings of this study are available within the article.

References

[1] Hu T, Pang XQ, Yu S, Wang XL, Pang H, Guo J, et al. Hydrocarbon generation and expulsion characteristics of lower Permian P1f source rocks in the Fengcheng area, northwest margin, Junggar basin, NW China: Implications for tight oil accumulation potential assessment. Geol J. 2015;51(6):880–900.10.1002/gj.2705Search in Google Scholar

[2] Zhou L, Pang X, Wu L, Kuang L, Pang H, Jiang F, et al. Petroleum generation and expulsion in middle Permian Lucaogou Formation, Jimusar sag, Junggar basin, northwest China: Assessment of shale oil resource potential. Geol J. 2017;52(6):1032–48.10.1002/gj.2868Search in Google Scholar

[3] Tang WB, Zhang YY, Pe-Piper G, Piper DJW, Guo ZJ, Li ZJ. Soft-sediment deformation structures in alkaline lake deposits of Lower Permian Fengcheng Formation, Junggar basin, NW China: Implications for syn-sedimentary tectonic activity. Sediment Geol. 2020;406(105719):1–19.10.1016/j.sedgeo.2020.105719Search in Google Scholar

[4] Li WW, Cao J, Zhi DM, Tang Y, He WJ, Wang TT, et al. Controls on shale oil accumulation in alkaline lacustrine settings: Late Paleozoic Fengcheng Formation, Mahu sag, northwestern Junggar basin. Mar Pet Geol. 2021;129(105107):1–17.10.1016/j.marpetgeo.2021.105107Search in Google Scholar

[5] Zhi DM, Tang Y, He WJ, Guo XG, Zheng ML, Huang LL. Orderly coexistence and accumulation models of conventional and unconventional hydrocarbons in Lower Permian Fengcheng Formation, Mahu sag, Junggar Basin. Pet Explor Dev. 2021;48(1):1–14.10.1016/S1876-3804(21)60004-6Search in Google Scholar

[6] Wu KY, Zha M, Wang XL, Qu JX, Chen X. Further research on the tectonic evolution and dynamic setting of the Junggar basin. Acta Geosci Sin. 2005;26(3):217–22 (in Chinese with English abstract).Search in Google Scholar

[7] Tao H, Wang Q, Yang X, Lin J. Provenance and tectonic setting of late Carboniferous clastic rocks in west Junggar, Xinjiang, China: A case from the Halaalat mountains. J Asian Earth Sci. 2013;64:210–22.10.1016/j.jseaes.2012.12.019Search in Google Scholar

[8] Feng JW, Dai JS, Li X, Luo P. Soft collision and polyphasic tectonic evolution of Wuxia foreland thrust belt: Evidence from geochemistry and geophysics at the northwestern margin of the Junggar basin. J Geodyn. 2018;118:32–48.10.1016/j.jog.2018.05.004Search in Google Scholar

[9] Zheng ML, Fan XD, He WJ, Yang TY, Tang Y, Ding J, et al. Superposition and evolution of deep geological structure and hydrocarbon accumulation in Junggar basin. Earth Sci Front. 2019;26(1):22–32 (in Chinese with English abstract).Search in Google Scholar

[10] Zheng ML, Tian AJ, Yang TY, He WJ, Chen L, Wu HS, et al. Structural evolution and hydrocarbon accumulation in the eastern Junggar Basin. Oil Gas Geol. 2018;39(5):907–17 (in Chinese with English abstract).Search in Google Scholar

[11] Bai ZH, Sun PY, Sun BC. The structural characters and its implications for hydrocarbon accumulation in Wuxia fault belt, Junggar basin. Pet Geol Eng. 2011;25(3):19–22 (in Chinese with English abstract).Search in Google Scholar

[12] Feng JW, Dai JS, Ge SQ. Structural evolution and pool-forming in Wuxia fault belt of Junggar basin. J China Univ Pet. 2008;32(3):23–9 (in Chinese with English abstract).Search in Google Scholar

[13] Ma DL, He DF, Di L, Tang JY, Zheng L. Kinematics of syn-tectonic unconformities and implications for the tectonic evolution of the Halaalat Mountains at the northwestern margin of the Junggar basin, central Asian Orogenic Belt. Geosci Front. 2015;6(2):247–64.10.1016/j.gsf.2014.07.004Search in Google Scholar

[14] Wang J, Dai JS, Feng JW, Huo LL, Shen DY. Evolution of structural style in Wuxia fault belt in Junggar basin. J Southwest Pet Univ. 2009;31(3):29–33 (in Chinese with English abstract).Search in Google Scholar

[15] Wang JW, Liao W, Zeng ZP, Zhao LQ, Cao JJ, Guo RC, et al. Development characteristics and geometric pattern analysis of compression-torsion fault zone in the Wuxia area of Junggar basin. Pet Geol Recov Effic. 2020;27(6):1–10 (in Chinese with English abstract).Search in Google Scholar

[16] Xu XW, Li XH, Jiang N, Li QL, Qu X, Yang YH, et al. Basement nature and origin of the Junggar terrane: New zircon U–Pb–Hf isotope evidence from Paleozoic rocks and their enclaves. Gondwana Res. 2015;28(1):288–310.10.1016/j.gr.2014.03.011Search in Google Scholar

[17] Lmin A, Zha M, Ding X, Bian B, Han C. Identification of a Permian foreland basin in the western Junggar basin (NW China) and its impact on hydrocarbon accumulation. J Pet Sci Eng. 2019;187:106810.10.1016/j.petrol.2019.106810Search in Google Scholar

[18] Bian WH, Hornung J, Liu ZH, Wang PJ, Hinderer M. Sedimentary and palaeoenvironmental evolution of the Junggar basin, Xinjiang, northwest China. Palaeobiodivers Palaeoenviron. 2010;90(3):175–86.10.1007/s12549-010-0038-9Search in Google Scholar

[19] Carroll AR, Lang YH, Graham SA, Xiao XC, Hendrix MS, Chu JX, et al. Junggar Basin, Northwest China, trapped late Palaeozoic ocean. Tectonophysics. 1990;181:1–14.10.1016/0040-1951(90)90004-RSearch in Google Scholar

[20] Chen X, Lu H, Shu L, Wang H, Zhang G. Study on tectonic evolution of Junggar Basin. Geol J China Univ. 2002;8(3):257–67 (in Chinese with English abstract).Search in Google Scholar

[21] Wang XJ, Song Y, Zheng ML, Guo XG, Wu HS, Ren HJ, et al. Tectonic evolution of and hydrocarbon accumulation in the western Junggar Basin. Earth Sci Front. 2022;29(6):188–205 (in Chinese with English abstract).Search in Google Scholar

[22] Charvet J, Shu LS, Laurent-Charvet S, Wang B, Faure M, Cluzel D, et al. Palaeozoic tectonic evolution of the Tianshan belt, NW China. Sci China Earth Sci. 2011;54(2):166–84.10.1007/s11430-010-4138-1Search in Google Scholar

[23] Li X, Lao HG, Hu QY, Zhao L. Tectonic evolution and its physical simulation of wuxia fault belt in the northwestern margin of Junggar basin. Pet Geol Exp. 2017;39(4):567–72 (in Chinese with English abstract).Search in Google Scholar

[24] He DF, Yin C, Du SK, Shi X, Ma HS. Characteristics of structural segmentation of foreland thrust belts: A case study of the fault belts in the northwestern margin of Junggar Basin. Earth Sci Front. 2004;11(3):91–101.Search in Google Scholar

[25] Lee KY. Geology of the Petroleum and Deposits in the Junggar Basin, Xinjiang Uygur autonomous region, Northwest China (Open-file report). US Geol Surv. 1985;53:85–230.10.3133/ofr85230Search in Google Scholar

[26] Zhu YH, Yan YM, Wang YM, Er C, Li YY. Study on sequence stratigraphy in clastic rocks and volcanics mixing accumulated formation: Taking Jiamuhe Formation in the northwestern margin of the Junggar basin as an example. Geosci. 2008;22(2):255–63 (in Chinese with English abstract).Search in Google Scholar

[27] Wang S, Wang G, Huang L, Song L, Huang Y. Logging evaluation of lamina structure and reservoir quality in shale oil reservoir of Fengcheng Formation in Mahu sag, China. Mar Pet Geol. 2021;133(105299):1–16.10.1016/j.marpetgeo.2021.105299Search in Google Scholar

[28] Yu K, Cao Y, Qiu L, Sun P, Jia X, Wan M. Geochemical characteristics and origin of sodium carbonates in a closed alkaline basin: The Lower Permian Fengcheng Formation in the Mahu sag, northwestern Junggar basin, China. Palaeogeogr Palaeoclimatol Palaeoecol. 2018;511:506–31.10.1016/j.palaeo.2018.09.015Search in Google Scholar

[29] Cao J, Xia L, Wang T, Zhi D, Li W. An alkaline lake in the Late Paleozoic Ice Age (LPIA): a review and new insights into paleoenvironment and hydrocarbon potential. Earth-Sci Rev. 2020;202(1):1–17.10.1016/j.earscirev.2020.103091Search in Google Scholar

[30] Zhu SF, Zhu XM, Niu HP, Han XF, Zhang YQ, You XC. Genetic mechanism of dolomitization in Fengcheng Formation in the Wuxia area of Junggar basin, China. Acta Geol Sin. 2012;86(2):447–61.10.1111/j.1755-6724.2012.00673.xSearch in Google Scholar

[31] Zhi DM, Tang Y, Zheng ML, Xu Y, Cao J, Ding J, et al. Geological characteristics and accumulation controlling factors of shale reservoirs in Fengcheng Formation, Mahu sag, Junggar Basin. China Pet Explor. 2019;24(05):615–23 (in Chinese with English abstract).Search in Google Scholar

[32] Zhu SF, Qin Y, Liu X, Wei CJ, Zhu XM, Zhang W. Origin of dolomitic rocks in the lower Permian Fengcheng Formation, Junggar basin, China: Evidence from petrology and geochemistry. Mineral Petrol. 2017;111(2):267–8.10.1007/s00710-016-0467-xSearch in Google Scholar

[33] Cao J, Yao S, Jin Z, Hu W, Zhang Y, Wang X, et al. Petroleum migration and mixing in the northwestern Junggar Basin (NW China): constraints from oil-bearing fluid inclusion analyses. Org Geochem. 2006;37:827–46.10.1016/j.orggeochem.2006.02.003Search in Google Scholar

[34] Wang XJ, Wang TT, Cao J. Basic characteristics and highly efficient hydrocarbon generation of alkaline-lacustrine source rocks in Fengcheng Formation of Mahu sag. Xinjiang Pet Geol. 2018;39(1):9–15 (in Chinese with English abstract).Search in Google Scholar

[35] Cao J, Zhang YJ, Hu WX, Yao SP, Wang XL, Zhang YQ, et al. The Permian hybrid petroleum system in the northwest margin of the Junggar Basin, northwest China. Mar Pet Geol. 2005;22(3):331–49.10.1016/j.marpetgeo.2005.01.005Search in Google Scholar

[36] Cheng SW. Oil-gas source and timing of hydrocarbon charging for Well Hashen2 in Halaalt area. Coal Technol. 2018;37(5):138–40 (in Chinese with English abstract).Search in Google Scholar

[37] Zhang SW. Identification and its petroleum geologic significance of the Fengcheng Formation source rocks in Halaalt area, the northern margin of Junggar basin. Oil Gas Geol. 2013;34(2):145–52 (in Chinese with English abstract).Search in Google Scholar

[38] Blanc JP, Allen MB, Inger S, Hassani H. Structural styles in the Zagros simple folded zone, Iran. J Geol Soc Lond. 2003;160(3):401–12.10.1144/0016-764902-110Search in Google Scholar

[39] Hou G, Sun S, Zheng C, Tang Y, Zhou L, Tao MO. Subsalt structural styles of Keshen section in Kelasu tectonic belt. Xinjiang Pet Geol. 2019;40(1):1–6.Search in Google Scholar

[40] Stockmal GS, Slingsby A, Waldron JW. Deformation styles at the Appalachian structural front, western Newfoundland: Implications of new industry seismic reflection data. Can J Earth Sci. 1998;35(11):1288–306.10.1139/e97-118Search in Google Scholar

[41] Ye T, Chen A, Hou M, Niu C, Wang Q. Characteristic of the Bodong segment of the Tanlu Fault Zone, Bohai sea area, eastern China: Implications for hydrocarbon exploration and regional tectonic evolution. J Pet Sci Eng. 2021;201:108478. 1–13.10.1016/j.petrol.2021.108478Search in Google Scholar

[42] Liu Y, Wang X, Wu K, Chen S, Shi Z, Yao W. Late Carboniferous seismic and volcanic record in the northwestern margin of the Junggar basin: Implication for the tectonic setting of the west Junggar. Gondwana Res. 2019;71:49–75.10.1016/j.gr.2019.01.013Search in Google Scholar

[43] Shi JJ, Chen XH, Ding WC, Li B. Late Paleozoic ocean-continent transition in west Junggar, central Asian orogenic belt: Evidence from late Carboniferous rhyolites. J Geomech. 2017;23(1):150–60 (in Chinese with English abstract).Search in Google Scholar

[44] Gao R, Long X, Wang GC, He XX, Yang G, Yan SW. Paleozoic magmatism and tectonic setting in West Junggar. Acta Pet Sin. 2013;29:3413–34 (in Chinese with English abstract).Search in Google Scholar

[45] Han B, Guo Z, Zhang Z, Zhang L, Chen J, Song B. Age, geochemistry, and tectonic implications of a Late Paleozoic stitching pluton in the North Tian Shan suture zone. Geol Soc Am Bull. 2010;122(3):627–40.10.1130/B26491.1Search in Google Scholar

[46] Li D, He DF, Lian YC, Lu Y, Yi ZJ. Structural evolution and late Carboniferous magmatism of the Zhongguai arc in the western Junggar Basin, Northwest China: implications for tectonic evolution of the Junggar Ocean. Int Geol Rev. 2017;59:1222–34.10.1080/00206814.2016.1160801Search in Google Scholar

[47] Chen S, Zhang Y. Tectonic Evolution of the Junggar Foreland Basin in the Late Carboniferous-Permian. Acta Geol Sin. 2001;75(4):398–408.10.1111/j.1755-6724.2001.tb00058.xSearch in Google Scholar

[48] Tang WB, Zhang YY, Pe-Piper G, Piper DJW, Guo ZJ, Li W. Permian to early Triassic tectono-sedimentary evolution of the Mahu sag, Junggar basin, western China: sedimentological implications of the transition from rifting to tectonic inversion. Mar Pet Geol. 2021;123:104730.10.1016/j.marpetgeo.2020.104730Search in Google Scholar

[49] Xiang B, Li E, Gao X, Wang M, Wang Y, Xu H, et al. Petroleum generation kinetics for Permian lacustrine source rocks in the Junggar Basin, NW China. Org Geochem. 2016;98:1–17.10.1016/j.orggeochem.2016.05.003Search in Google Scholar

[50] Ju W, Hou G, Zhang B. Insights into the damage zones in fault-bend folds from geomechanical models and field data. Tectonophysics. 2014;610:182–94.10.1016/j.tecto.2013.11.022Search in Google Scholar

[51] Ju W, Sun WF. Tectonic fractures in the lower Cretaceous Xiagou Formation of Qingxi oilfield, Jiuxi basin, NW China Part one: characteristics and controlling factors. J Pet Sci Eng. 2016;146:617–25.10.1016/j.petrol.2016.07.042Search in Google Scholar

[52] Sun S, Hou G, Zheng C. Fracture zones constrained by neutral surfaces in a fault-related fold: Insights from the Kelasu tectonic zone, Kuqa depression. J Struct Geol. 2017;104:112–24.10.1016/j.jsg.2017.10.005Search in Google Scholar

[53] Sun S, Hou G, Zheng C. Prediction of tensile fractures in KS2 trap, Kuqa Depression, NW China. Mar Pet Geol. 2019;101:108–16.10.1016/j.marpetgeo.2018.11.037Search in Google Scholar

[54] Wu KY. Research on the stages of reservoir formation in Wuerhe-Xiazijie area in Junggar basin. J Oil Gas Technol. 2009;31(3):18–23 (in Chinese with English abstract).Search in Google Scholar

Received: 2022-10-08

Revised: 2022-11-29

Accepted: 2022-12-19

Published Online: 2023-02-13

This work is licensed under the Creative Commons Attribution 4.0 International License.

Articles in the same Issue

https://doi.org/10.1515/geo-2022-0452

Keywords for this article

structure style; hydrocarbon accumulation; Fengcheng Formation; Wuxia fault belt; Junggar basin; foreland basin

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