Geological Characteristics and Controlling Factors of Enrichment of Deep Shale Gas in the East Weiyuan–North Rongchang Area, Sichuan Basin, China
Yijia Wu
Hongming Tang1* - 1School of Geoscience and Technology, Southwest Petroleum University, Chengdu, China
- 2Institute of Geological Exploration and Development of CNPC Chuanqing Drilling Engineering, Chengdu, China
The southern Sichuan Basin is the core area of China’s efficient development of deep shale gas (burial depth greater than 3,500 m). Reservoir geological characteristics determine whether shale gas can be preserved, enriched, and produced. Taking the Long 11 sub-member of the Wufeng Formation of the Upper Ordovician and the Longmaxi Formation of the Lower Silurian in the East Weiyuan–North Rongchang area as an example, we used the core, logging, production test, and other data, combining X-ray diffraction analysis, LECO Total Organic Carbon (TOC)-S analysis, optical microscopy, and argon ion polishing field-emission scanning electron microscopy, to study the shale mineral composition, geochemistry, reservoir space, pore structure characteristics, and reservoir physical properties. The following results were obtained: 1) The brittle mineral content, organic matter maturity, and TOC content are high, gradually increase from top to bottom, and reach their maxima at small layer 1 of Long 11. 2) Organic pores, inorganic pores, and fractures are important reservoir spaces, among which organic pores and fractures are important seepage channels for shale gas. 3) The shale pore structure revealed by electron microscopy shows that the pore structure in target layers can be divided into four types: unimodal type (mainly organic pores), bimodal type (both organic and inorganic pores), monoclinic type I (mainly organic pores), and monoclinic type II (mainly inorganic pores). The pore morphology is complex, and circular and oval shapes predominate. 4) Sedimentary facies are the main factor controlling the enrichment of shale gas, and the development of fractures is the key to obtaining high yields of shale gas. 5) The class I favorable target area is mainly distributed in wells W206, W206H1, R234H, and R233H and areas to its south, and some areas in the east of the study area.
Introduction
The marine shale gas resources in China are abundant. Reservoir geological characteristics have always been a hot topic in shale gas exploration and development in China and abroad since they play an important role in controlling the enrichment and production of shale gas (Fan et al., 2018; Li et al., 2019; Fan et al., 2020a; Fan et al., 2020b; He et al., 2021a). The favorable areas for marine shale gas are mainly located in Sichuan Basin, China. The main strata are the Wufeng Formation of the Upper Ordovician–Longmaxi Formation of the Lower Silurian, the main burial depth being 3,500–4,500 m. Shale gas areas have been found successively, such as Luzhou, Changning, Weiyuan, Fuling, and Dingshan, and breakthroughs in exploration and development have been made. The proven geological reserves in China are approximately 2.0 × 1012 m3. Their output is approximately 154 × 108 m3, making China the second-largest shale gas producer in the world (Nie and Jin, 2016; Nie et al., 2018; Zhang F. et al., 2020; He et al., 2021b).
The shale gas exploration technology for burial depths less than 3,500 m is well developed, forming a comprehensive geological evaluation technology of shale reservoirs that effectively guides the large-scale industrial development of medium–shallow shale gas. With the deepening of shale gas exploration and development, deep shale with burial depth greater than 3,500 m is widely distributed, with extensive resources (for example, the amount of deep shale gas in southern Sichuan is as high as 8 × 1012 m3) (Liu Y. J. et al., 2021; Li W. G. et al., 2021; Liu Y. Y. et al., 2021; Ma et al., 2021). Therefore, the development of geological theories related to the enrichment and production of deep shale gas has strategic significance for ensuring national energy security. Compared with shallow shale gas fields, there are obvious differences in geological engineering conditions of deep shale gas fields in China. For example, deep shale gas fields are mostly located in complex structural areas, with complex fold and fault relations, large in situ stress and stress differences, and high temperatures and pressures, so the main technologies suitable for shallow shale gas exploration and development are no longer adequate (Zhao et al., 2020; Zhang BL. et al., 2020, Zhang DD. et al., 2020; Xu F. S. et al., 2021; Xi et al., 2021a, Xi et al., 2021b). Previous studies have made great progress in understanding the geological characteristics of shale reservoirs; defined the geochemical characteristics, mineralogical characteristics, and reservoir space characteristics of the reservoirs; found that the sedimentary environment, organic matter (OM), clay minerals, brittle minerals, and fractures are the main controlling factors of shale reservoir yields; and formed a comprehensive research system for shale reservoirs (Chen et al., 2016; Li et al., 2019c; Chen S. L. et al., 2020; Li et al., 2020; Liu et al., 2020; Chen et al., 2021a; Chen et al., 2021b; Liu J. et al., 2021; Sun, 2021). However, these research results and conclusions apply mainly to shallow shale gas with a burial depth of less than 3,500 m. Due to the influence of sedimentation, diagenesis, and tectonism, deep shale gas reservoirs have higher contents of brittle minerals, more developed natural fractures, and more complex pore evolution, resulting in different shale geological characteristics and controlling factors for shale gas enrichment and yield (Yin et al., 2019; Chen F. et al., 2020; Chai et al., 2020; Xu and Gao, 2020; Yin and Wu, 2020; Zhou et al., 2020; Song et al., 2021; Tabatabaei 2021). Therefore, clarifying the geological characteristics of deep shale is needed to explore and extract deep shale gas.
The burial depth of the main shale in the East Weiyuan–North Rongchang area is 3,800–4,300 m, so the shale reservoir characteristics and the state of the shale gas and its preservation conditions are significantly different from those of medium–shallow shale gas. It is a typical area to analyze the geological characteristics and controlling factors of deep shale gas (Xiong et al., 2021; Zhao et al., 2021; Zhou et al., 2021). Therefore, we used the data from logging, core, seismic, and experimental tests to comprehensively analyze the rock and mineral characteristics, reservoir space characteristics, organic geochemical characteristics, and physical properties of high-quality deep shale reservoirs in the East Weiyuan–North Rongchang to clarify the main controlling factors of deep shale gas enrichment and high yield. We then calculated the optimal target areas, thus providing guidance for exploring and developing regional deep shale gas in this study area and similar areas.
Geological Setting
The East Weiyuan–North Rongchang block is located in the Central South of Sichuan Basin. The East Weiyuan block is located in the middle-slope gentle belt of the Central Sichuan Paleo-uplift and the low-fold belt of the Southwest Sichuan Paleo-uplift. North Rongchang block is located in the middle-slope gentle belt of Central Sichuan Paleo-uplift and the low steep bend belt of the Central Sichuan Paleo-depression. The structure of the study area is relatively simple. The Northern and Western areas consist of gentle, low-amplitude, monoclinic, or nasal protrusion-like structures, with undeveloped faults, and only some small-scale faults are developed. The Zhongaoxi buried structure is in the middle, the Luoguanshan structure is in the south, and the Xishan structure is connected in the east, showing the structural characteristics of a wide syncline and a narrow anticline. Faults are developed and mostly distributed in the NE–SW direction (Figure 1) (Wu et al., 2021; Zhao et al., 2021). The Late Ordovician–Early Silurian is the turning period of sedimentary-tectonic evolution of the Yangtze Block. Dominated by rising sea level, the East Weiyuan–North Rongchang area forms a detention basin, which inundates the carbonate platform and provides conditions for the deposition of black shale of the Ordovician Wufeng Formation and the Longmaxi Formation at the bottom of the Lower Silurian. Overall, the Wufeng Formation–Longmaxi Formation is mainly continental shelf facies in the study area. The shelf environment consists of an inner shelf close to the shore and far away. The upper limit is near the normal wave level, and the lower water depth limit is generally approximately 200 m (Liu S. G. et al., 2021; Liu Q. Y. et al., 2021). The Wufeng Formation–Longmaxi Formation is close to the shore facies in the landward direction on the plane, and the sediments are mainly dark mud debris.
FIGURE 1. Seismic reflection structure of the Upper Ordovician top boundary in the study area.
The oldest stratum exposed on the surface of the study area is the 1 Triassic Xujiahe formation, and the top is the Shaximiao Formation. The drilling data show that the stratigraphic sequence from top to bottom is normal. The stratigraphic thickness of the Lower Silurian Longmaxi Formation is 283–515 m, which is in conformable contact with the overlying Shiniulan Formation. At the bottom, there is a clear boundary between the black carbonaceous shale containing carbonate rock and the grayish-brown biological limestone of the Guanyinqiao Section of the Wufeng Formation of the Lower Ordovician, forming a pseudo-conformable contact. The rock color gradually deepens from top to bottom. The upper part is grayish-green and greenish-gray shale. The middle and lower parts are grayish-black to black calcareous and carbonaceous shale, which generally is calcareous, silty, dense, and brittle, and the foliation is relatively developed (leaf bedding). The natural gamma ray is serrated, mostly with high values. The bottom is obviously uplifted compared with the upper part, with a value of 140–500 API. The Longmaxi Formation can be divided into upper and lower segments, namely, the Long 1 member and the Long 2 member. The Long 1 member can be divided into upper and lower subsegments, namely, Long 12 and long 11. Long 11 can be divided into four small layers, the main shale gas-producing layers (Figure 2).
FIGURE 2. Comprehensive histogram of the Longmaxi Formation of well W206.
Samples and Experiments
Experimental Samples
The shale of the Wufeng Formation–Longmaxi Formation in the East Weiyuan–North Rongchang block was deposited in an organic-rich shelf environment (Wu et al., 2021; Zhao et al., 2021). In this study, conventional logging and imaging logging data of eight wells, including R202, R233H, W231, W232, and W206, were collected to analyze the characteristics of the reservoir lithology, reservoir space, brittle minerals, and gas-bearing. At the same time, 52 samples of five wells of Long 11 sub-member were collected, including 10 shales in small layer 1, 15 shales in small layer 2, eight shale in small layer 3, and 19 shales in small layer 4.
X-Ray Diffraction Analysis
The 52 samples were crushed and passed through a 200-mesh sieve. After drying, a certain number of samples were taken and analyzed by a Bruker D8 X-ray diffractometer. The working voltage was 40 kV, the current was 30 mA, and the scanning was conducted at 4°/min. Determinations were made according to the Inorganic chemicals for industrial use-Crystal form analysis-X-ray diffraction method (GB/T 30904-2014). The main peak area of each mineral was used to calculate the relative content (Cai et al., 2020).
Geochemical Characteristic Analysis
The OM maturity and abundance are key geochemical characteristics of shale. Since there is no vitrinite in the highly mature source rocks of the Lower Paleozoic, the maturity of the Lower Paleozoic source rocks cannot be evaluated by vitrinite reflectance (Shi et al., 2016; Yu H. et al., 2017; Rui et al., 2019; Wang et al., 2019). In this study, the maturity of the Lower Paleozoic source rocks was evaluated by studying the correlation between solid asphalt and vitrinite reflectance, fitting the conversion formula between asphalt reflectance and vitrinite reflectance, and converting the asphalt reflectance into vitrinite reflectance.
Total organic carbon (TOC) content can better characterize the OM abundance. In this study, 52 samples were crushed and passed through a 200-mesh sieve. After drying at low temperature, the carbonate minerals were removed with dilute hydrochloric acid. According to the Determination of total organic carbon in sedimentary rock (GB/T 19145-2003), the TOC content was determined with a LECO CS230 carbon/sulfur determinator (Wang et al., 2016; Zhao et al., 2017; Cai et al., 2020).
Observation by Argon Ion Polishing Field-Emission Scanning Electron Microscopy
Representative core samples from five wells were selected for SEM observation according to our core observation. First, the experimental samples were polished by argon-ion, and then small shale samples were cut into regular cuboids and put into the injection chamber of the polisher. They were bombarded with argon ions in a vacuum for 2 h, and then the SU8010 FESEM has used under the secondary electron (SE)/backscattered electron (BSE) mode. The observation was carried out to obtain images of complete shales.
Results
Mineral Composition Characteristics
The XRD analysis of the first segment of the Wufeng Formation–Longmaxi Formation in the study area shows that minerals are mainly quartz, feldspar, calcite, dolomite, and clay minerals, and pyrite and marcasite contents are scarce. The brittle minerals are primarily quartz, feldspar, carbonate minerals, pyrite, and hematite, showing a gradually increasing trend from top to bottom in the vertical direction, and the content of brittle minerals peaks at small layer 1 (Figures 3A,B). Specifically, the content of brittle minerals in the Wufeng Formation is 62.6–89.9%, with an average of 74.9%; in small layer 1, 55.3–76.4% with an average of 64.4%; in small layer 2, 60.3–79% with an average of 67.5%; in small layer 3, 49.9–74.5% with an average of 60.2%; and in small layer 4, 45.2–72% with an average of 58.3% (Figure 3C). In terms of plane distribution, each well’s measured brittle mineral content is generally stable, with an average greater than 60%. The brittle mineral content of the Wufeng Formation Long 11 sub-member reservoir increases in the east and south directions. The high-value area is distributed from well W206-H2 to well R202, the content gradually decreases toward the surrounding well area, Well W231 is a relatively low-value area, and the compressibility of shale reservoir is generally good (Zhou et al., 2016; Zhang et al., 2019; Zhu et al., 2019; Zhang et al., 2021).
FIGURE 3. Mineral composition in Wufeng Formation Long 11 sub-member in the study area. (A). R233H. (B). Well W206-H2. (C). Brittle mineral content in the study area and adjacent areas.
Geochemical Characteristics
The observation of cores and thin sections shows that there is no vitrinite in the highly mature source rocks of the Lower Paleozoic in the study area, only solid asphalt, which is the residue left after the gas generation of crude oil (He X. et al., 2021; He et al., 2021d; Yuan et al., 2021). Therefore, according to the correlation between solid asphalt and vitrinite reflectance, the maturity of the Lower Paleozoic source rocks can be evaluated after converting asphalt reflectance into vitrinite reflectance. Based on the empirical OM maturity measured by two core analysis methods, the average asphalt reflectance converted into Ro in Long 11 is 2.2%. The measured average Ro of graptolite reflectance is 3.1%, and both are over mature stages, mainly producing dry gas (Table 1).
TABLE 1. OM maturity in the core analysis of sub-member Long 11 in the study area.
To characterize shale OM abundance quantitatively, the LECO CS230 carbon/sulfur analyzer was used to determine the TOC content of gas-bearing shale from Wufeng Formation Long 11. The empirical analysis shows that the average TOC of each small layer of Long 11 and the Wufeng Formation core is 0.5–2.88%, with small layer 1 having the highest 5.18% (Figure 4). Consistent with shallow shale gas, small layer 1 has the highest thermal evolution and OM abundance.
FIGURE 4. Analysis of TOC content of each small layer by core of the Wufeng Formation Long 11 sub-member in the study area.
Reservoir Space Characteristics
According to the observation of thin cast sections and the AIP-FESEM of typical samples from five coring wells in the study area, the main reservoir space types of the Wufeng Formation Long 11 are organic pores, inorganic pores, and fractures. OM forms organic pores in the later thermal evolution process. Inorganic pores can be further divided into six types (Intergranular pore, Micropore in clay minerals, Intragranular dissolved pore, Intracrystalline dissolved pores, Biological pore, OM pore), mainly including intergranular pores, intercrystalline dissolved pores, and intergranular pores. Fractures mainly include structural and nonstructural fractures, whose development degree is related to the thermal evolution degree of OM, shale brittleness, and tectonic stress. The pore types are mainly micro-nano-pores (Jarvie et al., 2007; Curtis et al., 2012; Zhang K. et al., 2020; Rashid et al., 2020; Xiao et al., 2020; Huang et al., 2021).
1) OM pores
OM pores are the main pore type of shale gas reservoirs. OM pores and their specific surface provide an adsorbent for natural gas and a space for the occurrence of free gas, which is very important for the enrichment of shale gas (Sakhaee-Pour and Bryant, 2015; Guo et al., 2018; Han et al., 2019; Ko, et al., 2017). The development of OM pores is affected by the degree of thermal evolution and the microstructure of the OM, resulting in great differences in the distribution patterns of OM pores in a single vertical well. The study area has a high degree of the thermal evolution of OM. OM pores in various forms are widely distributed. Circular and oval shapes predominate inside them, and sponge, though pore and strip shapes are observed. The pores are irregular, uneven distribution, and the pore diameter is mainly less than 50 nm (Figures 5A–C). Longitudinally, the TOC of small layer 1 is the highest, mainly as a sapropel formation, and the developmental degree of OM pores is significantly greater than that of other small layers.
2) Intergranular pores
FIGURE 5. Reservoir space types and characteristics of the Long 11 sub-member in the study area. (A). W206, 3,787.53 m, Micropores in organic matter. (B). W206, 3,765.52 m, Micropores in organic matter. (C). R233H, 3,884.35 m, Organic matter pore, The pores are round-oval. (D). W206H2, 3,782.52 m, The intergranular pores are lamellar. (E). W206, 3,771.81 m, Flaky intergranular pores between clay particles. (F). W206, 3,781.76 m, intergranular pores. (G). W206, 3,787.53 m, Intercrystalline pores in pyrite particles. (H). W231, 3,878.92 m, Intercrystalline pores in pyrite particles. (I). R233H, 3,893.50 m, Intercrystalline dissolved pores. (J). W231, 3,878.85 m, Vertical fracture, unfilled. k. R233H, 3,885.27 m, Calcite can be seen on the fracture surface, and there are scratches on the fracture surface. (L). W206, 3,753.86 m, Microcracks parallel to clay bedding. (M,N), characteristics of bedding fractures in the imaging logging. (O). R233H, 3,879.27 m, grain edge fractures. (P). W231, 3,856.62 m, grain edge fractures of organic matter.
Compared with conventional oil and gas reservoirs, shale reservoirs have a shallow burial depth and relatively low compaction and diagenesis, and they retain more intergranular pores. Irregular dissolved pores, including mold pores, are formed in feldspar, calcite, dolomite, and other particles. During diagenesis, compaction, and cementation, due to incomplete action, intergranular pores can develop around ductile minerals (clay flocs, microcrystalline spherulite minerals, OM, etc.) and brittle minerals (quartz, feldspar, pyrite, etc.). The pore types are linear and triangular, and the pores are generally larger than OM pores (Figures 5D–F).
3) Intercrystalline pores/Intercrystalline dissolved pores
Due to the irregularity of the crystals, brittle and compressive particles, such as pyrite, carbonate, and quartz, it easily form intercrystalline pores in the process of crystal packing in the study area. They are mainly includes pores developed between authigenic crystals, and the pores are clean. Most of these pores are isolated and poorly connected, so it is difficult for natural gas in the source area to flow into these pores (Zou et al., 2010; Yu et al., 2016, Yu Y. X. et al., 2017). Pyrite microspheres formed under an anoxic environment are widely distributed in the study area, present as aggregates of pyrite crystals in a raspberry-like shape, and mostly exist individually as regular cube shapes. Due to the non-tight packing during the crystal growth process, the intercrystalline micropores are mostly irregular (Figures 5G,H). OM can form many organic acids in hydrocarbon generation, and there are some acidic substances in water formation (Lyu et al., 2021; Wang et al., 2021). These substances migrate under the action of potential energy. They can selectively dissolve feldspar, calcite, and other soluble minerals so that the intercrystalline pores are dissolved in varying degrees, thus forming intercrystalline dissolved pores dominated by ellipses and triangles (Figure 5I).
4) Fractures
Shale reservoirs are characterized by ultralow porosity and low permeability. The development of fractures affects the physical properties of shale reservoirs and strongly influences the formation and expansion of hydraulic pressure fractures, thus affecting shale productivity. Structural and nonstructural fractures are the main fractures developed in the study area (Zou et al., 2010; Li H. et al., 2021; Li, 2021). Structural fractures are mainly shear fractures formed by structural stress. Our core observation shows that most of them are low-angle and high-angle fractures characterized by flat and smooth fracture surfaces, a regular occurrence, far extension, and more clastic particles (Figures 5J,K). Similar characteristics were observed under the electron microscope. Such fractures can better connect poorly interconnected pores, thus greatly improving the seepage capacity of the reservoir (Figure 5L). However, if high-angle fractures develop through the layer, this may lead to the loss of shale gas, which is unfavorable to the preservation of shale gas. Foliation bedding fractures are also widely developed in the study area. These fractures show up as dark linear patterns on the map by imaging logging and are mainly the connected organic and inorganic pores in the shale. They can effectively increase the effective porosity of the reservoir, have a great influence on the horizontal seepage capacity of the reservoir (Figures 5M, N), and are an important weak surface for the expansion of compression fractures. In addition, microfractures in the study area are extremely well developed, with lengths usually ranging from micrometers to nanometers and widths ranging from hundreds of nanometers to several micrometers. These fractures are of structural origin and nonstructural origin. Fractures with structural origin have characteristics similar to macro-shear fractures (Figure 5L), and fractures with nonstructural origin are mainly developed along weak planes dominated by bedding planes and lithologic interfaces, primarily coming in three types: 1) cleavage fractures formed in flake minerals; 2) grain edge fractures formed at the interface between clay minerals and clastic particles (Figures 5O, P); and 3) intercrystalline fractures of clay minerals, quartz particles, and pyrite. These microfractures are intertwined into a network, and the joint action of micro-and macro fractures has an important impact on the enrichment of shale gas.
Overall, the shale reservoir space of the Longmaxi Formation in the study area is mainly composed of organic pores, inorganic pores, and fractures. Due to the multistage tectonic stress of Indosinian, Yanshan, and Himalayan orogenies, the shale of the Longmaxi Formation has the characteristics of obvious compaction and diagenesis, a high degree of thermal evolution, strong tectonic uplift, and deep burial depth, so OM well-connected pores and fractures are developed in the study area. In contrast, inorganic pores are less developed and poorly connected. Therefore, in the study area, OM pores and fractures are important seepage channels of shale gas.
Pore Structure Characteristics
The SEM analysis of shale pore structure shows that the pore structure of shale reservoirs in the Wufeng Formation Long 1 Member gradually improves from top to bottom. In contrast, the proportion of mesopores (2–50 nm) and large pores (>50 nm) increases, but small pores (<2 nm) and mesopores still predominate, accounting for 42 and 49%, respectively. According to the frequency distribution curve of pore radius, pore structure can be divided into four types (Xiong et al., 2021), i.e., unimodal (mainly organic pores), bimodal (both organic and inorganic pores), monoclinic type I (mainly organic pores), and monoclinic type II (mainly inorganic pores). Their characteristics are as follows.
Unimodal type: There is only one peak frequency of the pore radius. The pore radius has a narrow distribution range, and small pores (micropores) less than 2 nm predominate and are rich in OM (TOC≥4.5%). The lithology is mainly calcareous-clay-siliceous mixed shale. More than 60% of the pores are OM pores. Intergranular pores and intergranular pores are rare, the pores have good sortability and connectivity, and the reservoir has good physical properties (Figure 6A). The pore morphology is mainly circular, elliptical, or irregular, together accounting for more than 85%. The pores of other shapes, such as narrow, long, and wedge-shaped, are relatively developed, accounting for approximately 15% (Figure 6B).
FIGURE 6. Distribution characteristics of pore structure based on the SEM. (A) Pore radius curve characteristics of the unimodal type. (B) Pore morphological characteristics of the unimodal type. (C) Pore radius curve characteristics of the bimodal type. (D) Pore morphological characteristics of the bimodal type. (E) Pore radius curve characteristics of the monoclinic type I. (F) Pore morphological characteristics of the monoclinic type I. (G) Pore radius curve characteristics of the monoclinic type II. (H) Pore morphological characteristics of the monoclinic type II.
Bimodal type: There is one peak frequency for the pore radius, the difference between primary and secondary peaks is large, the main peak is approximately 0.1–0.2 μm, and the secondary peak is about 1–10 μm. Pore size varies widely, and mesopores and large pores predominate, with relatively poor sortability and strong heterogeneity. Both organic and inorganic pores are developed, accounting for the same proportion (40–50%), the TOC content is between 2.5 and 3.5%, and the brittle mineral content is high. The organic pore distribution is uneven, the connectivity in general, and the pore structure is slightly worse than that of the unimodal type (Figure 6C). The pore morphology is circular and elliptical, accounting for approximately 75%. The proportion of other forms is relatively low, explained by the good compression resistance of rigid particles (Figure 6D).
Monoclinic type I: Organic pores predominate, inorganic pores are not developed, and the pore radii are mostly 0.05–0.1 μm. The mesopores predominate, have good sortability, and are rich in OM (TOC≥4.5%). The lithology is mainly biological siliceous shale, and pyrite laminae are developed. The pore morphology is mainly circular or oval, accounting for approximately 60%, while irregular, narrow, and wedge-shaped pores account for more than 35%. Siliceous shale has the highest content, the pore radius of organic pores is better than that of unimodal type, and these reservoirs have the best physical properties (Figures 6E,F).
Monoclinic Type II: Inorganic pores predominate, organic pores are not developed, and the pore radii are mostly 0.01–0.02 μm. Small pores predominate, with good sortability but poor connectivity and low OM content (TOC<2%). The content of clayey shale is high, pyrite is rare, and round or oval pores account for approximately 55%. They have poor connectivity (Figures 6G,H).
Physical Characteristics
Based on the core analysis, vertically, the average core porosity of Long 12, each small layer of Long 11, and the whole Wufeng Formation is 6.24%, of which small layer 1 has the highest core porosity (7.06%) and Wufeng Formation the lowest (5.77%) (Figures 7A,B). Overall, core porosity gradually decreases from bottom to top. The core permeability is 1.33–3.32 × 10−4 MD, small layer 1 having the highest and Wufeng Formation the lowest (Figure 7C).
FIGURE 7. Distribution of porosity and permeability of the Wufeng Formation Long 11sub-member in the study area. (A) Porosity of each sub-member. (B) Porosity of the single well. (C) Permeability of each sub-member. (D) Permeability of the single well.
The logging results show that the porosity of the Wufeng Formation Long 11 sub-member of eight wells in the study area is 4.7–6.0%, with an average of 5.5%. Well W206-H1 had the lowest, Well W206 had the highest, and the distribution is mainly within 5.6–5.8%. Vertically, the porosity trend of each small layer of each well is about the same, of which small layer 3 and small layer 1 have the highest porosity, with an average of 5.84 and 5.68%, respectively, and Wufeng Formation has the lowest, with an average of 4.52% (Figure 7D).
The porosity decreases eastward and southward away from the denudation line in the plane distribution. The reservoir area with high porosity is distributed along with the wells W206-H2-R233H-HS1, and well W231 is a relatively low-value area; the reservoir areas with high porosity in small layer 1 are in wells W206, W205 to the northwest, and well WL203 to the south. Overall, the porosity increases with greater formation burial depth and gradually decreases to the south.
Discussion
Controlling Factors of Deep Shale Gas Enrichment and Yield
Sedimentary Facies Are the Main Factor Controlling the Development of Shale Gas Reservoirs
1) An anoxic deep-water strongly reducing environment is a necessary condition for OM enrichment
The reducibility of sedimentary water strongly affects the preservation of OM, and an anoxic strong reduction environment is more conducive to the enrichment and preservation of OM (Loucks et al., 2009; Cheng et al., 2021). Trace element analysis showed that the U/Th ratio of the small layer 1 is > 1.25, making it a strongly reducing environment of residual hypoxia, an important and favorable feature for sweet-spot layers. The core analysis data show good positive correlations between TOC and the V/Cr, U/Th, and Ni/Co values of trace elements, with corresponding coefficients of determination (R2) of 0.4141, 0.4794, and 0.6418 (Figure 8). The higher the R2, the more anoxic the sedimentary environment of the formation will be, and the more OM will be enriched.
2) The OM content and maturity are the key factors affecting the physical properties and gas-bearing of shale gas reservoirs
FIGURE 8. Relationship between TOC content and V/Cr, U/TH, and Ni/CO in the study area.
OM is the material source of shale gas. Thermal maturation makes OM generate many hydrocarbons after reaching the hydrocarbon generation threshold. After OM generates hydrocarbon, it begets high-pressure protective pores and forms organic pores in the process of hydrocarbon generation, which increases the rock’s porosity. At the same time, the reduction in OM volume could produce ultrafine fractures, which is conducive to the preservation of shale gas. Many micropores and microfractures are generated in the process of hydrocarbon generation, and more free natural gas is stored in these spaces. The higher the TOC content, the larger the total volume of pores, and the larger the specific surface area available for adsorption of adsorbed gas. Thus, the total gas volume of the shale will grow. The core analysis and test data of 11 wells (including W203, W205, W206, and R233H) show that the TOC content has positive correlations with porosity, quartz, and gas content (Figure 9), which also confirms the positive role of OM in shale reservoir space and gas-bearing property.
3) Organic rich siliceous mud shelves and organic-rich mud shelves are the most favorable sedimentary microfacies for shale gas enrichment
FIGURE 9. Relationships between TOC content and porosity, gas volume, and quartz in the study area.
The results of sedimentary microfacies analysis show that deep-water silty mud shelves, organic-rich silty mud shelves, organic-rich siliceous mud shelves, and organic-rich mud shelves in the outer shelf subfacies are the favorable microfacies for shale gas exploration and development. Among them, organic-rich siliceous mud shelves and organic-rich mud shelves are the most favorable microfacies owing to the following characteristics: high TOC content, with an average of 5%, giving them better hydrocarbon generation potential and more abundant shale gas resources; more developed pores, with an average porosity of 6%, providing enough reservoir space for shale gas enrichment; more developed shale interlayer foliation fractures; medium-carbon and high-carbon siliceous shale facies with their high brittle mineral contents and low carbonate mineral contents (mostly less than 10%); a high biogenic silica content, greater than 45%, which is conducive to improving the hydrofracture effect of shale (Table 2).
TABLE 2. Sedimentary microfacies of the first member of the wufeng formation–longmaxi formation in the study area.
Fracture Development Is the Key Factor for Achieving a High Yield of Shale Gas
Fractures are important reservoir spaces and migration channels of shale gas, playing an important role in the accumulation, preservation, exploration, and development of shale gas (Li et al., 2019c; Li et al., 2020; Li H. et al., 2021; Li 2021). Investigation of the Lower Paleozoic marine shale gas in the Sichuan Basin and its surrounding areas shows that marine shale has a good material foundation, and gas-bearing can almost be observed in each drilling. Still, the gas drilling results are very different. Therefore, the preservation conditions are key factors in determining whether shale gas can be enriched and produced. The shale gas area in North America is characterized by weak structural activity and developed horizontal fractures. Most of the shale gas is enriched in shale reservoirs uniformly (Figure 10A). Therefore, good single-well production can often be realized through fracturing and reconstruction of the reservoir. However, China’s shale gas enrichment modes are mainly anticlinal and synclinal structural modes, and both are found in the study area (Figures 10B,C). Therefore, fully sealing the top and floor of the reservoir is very important for reservoir formation, and the fracture is the key to the sealing effect. If the fracture or fault is not developed at the high point of the syncline or anticline structure, the shale gas may not be lost, and the fracture could play a positive role in the accumulation of shale gas. The shale gas of the anticline structure is accumulated in the core of the anticline, while the syncline structure is concentrated in the syncline wings.
FIGURE 10. Compound Controlling Mode of Structural Fractures in Shale Gas Reservoirs (Wang et al., 2017; Xu Z. et al., 2021). (A). Model diagram of a shale gas reservoir in North America, with weak structural activity and horizontal fractures. (B). Enrichment model of synclinal gas with no fractures developed at structural highs. (C). Enrichment model of anticlinal gas with no fractures developed at structural highs.
According to the correlation between the test product and the four property parameters of the reservoir in the study area, test production of less than 200,000 m3 in a well positively correlates with the reservoir’s physical properties. In contrast, the presence of a test production of more than 300,000 m3 has a poor correlation with the reservoir’s physical properties (Figures 11, 12). Therefore, the development of fractures is often a direct manifestation of the poor correlation with reservoir physical properties. As the gas test production is related to geological and engineering factors, geological factors determine the shale gas enrichment, and engineering factors play an important role in improving the test production. Different fracturing and mining methods will lead to different test production in the same area. Therefore, the correlation coefficient (R2) is small in Figures 11, 12, proving that their correlation is weak. The phenomenon is normal. In addition, according to the seismic prediction results of the fracture development zone, most of the class I wells with a test production of more than 300,000 m3 are located in areas with relatively well-developed fractures. The comparison between the test productivity data and the micro-seismic fracture monitoring data also shows that the test productivity of shale gas production wells in the fracture development area is generally larger than that in the area where fractures are not developed (Figure 13).
FIGURE 11. Relationship between test production below 200,000 m3 and reservoir physical properties in the study area.
FIGURE 12. Relationship between test production above 300,000 m3 and reservoir physical properties in the study area.
FIGURE 13. Relationship between fracture development area and test productivity.
Selection of Favorable Target Areas
According to the evaluation indices for choosing shale gas areas in China and abroad, combined with the existing research results in Southern Sichuan and the actual situation of the study area, seven evaluation parameters, such as gas volume, pressure coefficient, porosity, brittle mineral content, high-quality shale thickness, burial depth, and TOC, were selected as the main evaluation indices for the selection of favorable areas. The evaluation standards for determining shale gas areas in the study area were formulated (Table 3). The combination of these with the location parameters, such as structure, preservation conditions, burial depth, and class I + II reservoir thickness, the classification standards of favorable areas in the study area was formulated (Table 4), and finally, the study area was divided into class I, II, and III favorable areas (Figure 14).
TABLE 3. Comprehensive evaluation standard of selecting shale gas areas in the study area.
TABLE 4. Classification standards of favorable areas in the study area.
FIGURE 14. Favorable target areas in the study area.
Class I favorable areas are a class I + II reservoirs with a thickness of more than 40 m, a reservoir index of more than 1.4, undeveloped faults, and a relatively simple structure. They lack surface nonworking areas, have a burial depth of less than 4,000 m, and are mainly distributed in the south of wells W206, W206H1, R234H, R233H, and some areas in the east of the study area.
Class II favorable areas are the areas with reservoir thickness greater than 25 m, reservoir index greater than 1.2, undeveloped faults, and a relatively simple structure. They lack nonworking ground areas, have a burial depth of less than 4,500 m, and are mainly distributed in the north of well W206H1 in the middle of the study area, a belt running through the north and south of the area where Well W206H2 is located, and the northeast of North Rongchang block.
The class III favorable areas are those with reservoir thickness less than 25 m, either with or without fracture development. They are located in the Xishan/Luoguanshan structural belt, lack ground nonworking areas, are buried within a small layer at 4,500 m, and are mainly distributed in the northwest of well W232 and well W231 in the study area.
Conclusion
Taking the Long 11 sub-member of the Wufeng Formation of the Upper Ordovician and the Longmaxi Formation of the Lower Silurian in the East Weiyuan–North Rongchang area as an example, this paper comprehensively studies the geological characteristics and controlling factors of the enrichment and high-yield of deep shale gas by XRD analysis, LECO TOC-S analysis, optical microscopy, and AIP-FESEM and identified the favorable target areas for shale gas development in the study area. The main findings and conclusions are as follows:
1) In the study area, the brittle minerals of the Long 11 sub-member of the Wufeng Formation–Longmaxi Formation are mainly quartz, feldspar, carbonate minerals, pyrite, and hematite. The OM is in the over mature stage, and the TOC content is high, primarily producing dry gas. Vertically, the maturity of brittle minerals and OM and TOC contents gradually increases from top to bottom, the small layer 1 having the most.
2) The reservoir space of the Long 11 sub-member of the Wufeng Formation–Longmaxi Formation in the study area mainly includes organic pores, inorganic pores, and fractures. The inorganic pores are mainly intercrystalline, intercrystalline dissolved pores, and intergranular pores. Organic pores and fractures are important seepage channels of shale gas, and microfractures can better connect inorganic and organic pores. According to the frequency distribution curve of pore radii, the pore structure can be divided into the unimodal type, bimodal type, monoclinic type I, and monoclinic type II. The unimodal type is the best, with small pores predominating, followed by mesopores and the developed organic pores. The unimodal type has high OM content, good sortability, and good connectivity.
3) Considering the redox environment, sedimentary facies, lithofacies, reservoir characteristics, and other factors, the sedimentary facies is the main thing controlling the development of shale gas reservoirs in the study area. The organic-rich siliceous mud shelf microfacies, organic-rich mud shelf facies, and high-carbon siliceous shale facies deposited in deep-water strongly reducing environments are the most favorable areas for developing shale gas reservoirs. Under favorable reservoir conditions, the development of fractures is the key factor in obtaining high shale gas yields.
4) Combining the reservoir evaluation index, burial depth, class I + II reservoir distribution, and structural development in the study area, we identified the favorable exploration target areas in the study area. In the class I areas, the reservoir thickness is greater than 40 m, the reservoir index is greater than 1.4, the fault is not developed, and the structure is relatively simple. The class I areas are mainly distributed in W206, W206H1, R234H, and R233H and areas to its south and some areas in the east of the study area.
Data Availability Statement
The original contributions presented in the study are included in the article/supplementary material, further inquiries can be directed to the corresponding author.
Author Contributions
YW contributed in writing, reviewing, and editing, data curation, writing-original draft preparation; JL, ZG, BY, CY and TT contributed in formal analysis, validation, and methodology, supervision, project administration; HT contributed to visualization and investigation.
Conflict of Interest
The 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
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Keywords: deep shale gas, geological characteristics, reservoir characteristics, Enrichment and high yield, controlling factors, pore structure, East-Weiyuan-north Rongchang area
Citation: Wu Y, Tang H, Li J, Gao Z, Yang B, Yang C and Tang T (2022) Geological Characteristics and Controlling Factors of Enrichment of Deep Shale Gas in the East Weiyuan–North Rongchang Area, Sichuan Basin, China. Front. Earth Sci. 10:860952. doi: 10.3389/feart.2022.860952
Received: 24 January 2022; Accepted: 15 February 2022;
Published: 03 March 2022.
Edited by:
Shuai Yin, Xi’an Shiyou University, ChinaReviewed by:
Yue Qingyou, Liaoning Shihua University, ChinaYang Wang, China University of Petroleum, Beijing, China
Copyright © 2022 Wu, Tang, Li, Gao, Yang, Yang and Tang. 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: Yijia Wu, wuyj_dyy@cnpc.com.com; Hongming Tang, swpithm@vip.163.com