You Zhang
Qiang Li2- 1PetroChina Hangzhou Research Institute of Petroleum Geology, Hangzhou, China
- 2Exploration and Development Research Institute, PetroChina Daqing Oilfield Company, Daqing, China
- 3College of Resource and Environment, Henan Polytechnic University, Jiaozuo, China
- 4College of Geosciences, China University of Petroleum (Beijing), Beijing, China
- 5College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao, China
The heterogeneity of deep carbonate reservoirs is strong, it is significant for exploration and development to clarify the key stages of oil and gas accumulation. Taking the Ordovician in the Gucheng area of Tarim Basin as an example, this paper systematically investigated the key stage and model of hydrocarbon accumulation using the data of the cores, thin sections, cathode luminescence tests, laser ablation U-Pb isotope geochronometry, bitumen reflectance, and fluid inclusion tests, and seismic interpretation. (1) The Tarim Basin mainly develops three sets of effective source rocks, namely the Cambrian Yuertusi Formation, Cambrian Moheershan Formation, and Mid-Lower Ordovician Heituwa Formation, which are concentrated in the slope-basin facies of eastern Tarim Basin. (2) The Gucheng area is located in a favorable paleo-structural position. The pathway system composed of vertical faults and lateral unconformities occurs in the paleo-uplift, which is critical for hydrocarbon migration and accumulation. (3) The laser in-situ U-Pb dating, distribution and genesis of reservoir bitumen, burial-thermal maturation history, and the homogenization temperature of fluid inclusions suggest that the multi-stage tectonic thermal events of the Caledonian and Hercynian stages result in key adjustment and modification to deep hydrocarbon accumulation. Due to magmatic hydrothermal activities, the Caledonian primary oil reservoir massively evolved into oil-cracking gas reservoirs and residual paleo-oil reservoirs. (4) The paleo tectonic-fluid effect plays an important factor controlling the development of the Ordovician reservoirs. The evolution of the hydrocarbon accumulation in Gucheng area can be divided into three stages, namely formation of primary oil and gas reservoirs, oil-cracking gas reservoirs, and adjustment, destruction and reforming of gas reservoirs. To sum up, the western and northern parts of the paleo-uplift with favorable source-reservoir-cap rock assemblage and less effects of hydrothermal activities are the favorable zones for hydrocarbon exploration in the Gucheng area, the Tarim Basin.
1 Introduction
Over the recent years, significant breakthroughs have been continuously made in carbonate rocks of the marine facies, which has become the major strategic field for sustainable development of deep hydrocarbon exploration in China (Jia and Pang 2013; Sun et al., 2013; Dong et al., 2020; Li H et al., 2022). The Ordovician of the Gucheng area, Tarim Basin, is deposited in the slope belt of the carbonate platform-basin transition. Compared with that of the carbonate platform facies in the basin, it presents more diverse reservoir types and is closer to the Cambrian–Lower Ordovician source rock. Therefore, the Gucheng area is considered to be one of the areas in the Tarim Basin with the best conditions for hydrocarbon generation and storage (Shen et al., 2018; Zhang et al., 2018; Hong et al., 2020; Zhang et al., 2021). By the end of 2021, PetroChina had made massive physical efforts of two-(2D) and three-(3D) dimensional seismic prospecting and drilling across its 1.9 × 104 km2 lease area in the Gucheng area, and 18 prospecting wells have been drilled during the past 10 years. The exploration suffers from low success rates of prospecting wells, complex reservoirs, complicated conditions for hydrocarbon accumulation, the occurrence of pyrobitumen, and poor oil testing results due to poor reservoir porosity. A review of the whole exploration practice in eastern Tarim Basin reveals that hydrocarbon was discovered only in relatively limited areas, and no proven reserves have been submitted yet. Accordingly, doubts are raised regarding the exploration potential of the Lower Paleozoic carbonate rock of the Gucheng area of the eastern Tarim Basin.
Extensive work has been performed from numerous points of views, in terms of the stratigraphic sequence (Fan et al., 2007; Zhao et al., 2010; Lin et al., 2013; Zhao, 2015), lithofacies paleogeography (Feng et al., 2006; Feng et al., 2007; Liu et al., 2011; Zhang et al., 2015), structural–sedimentary evolution (Zhang et al., 2007; Han et al., 2009; Li Q et al., 2014; Wang G et al., 2014), characteristics and formation mechanisms of reservoir rocks (Zheng et al., 2016; Shao et al., 2019), and control factors of hydrocarbon accumulation and exploration fields (Cao et al., 2019; Lv et al., 2022; Tochukwu et al., 2022), and some commonly accepted basic understandings have been obtained. For instance, the hydrocarbon exploration in the Tarim Basin shall highlight the Gucheng area with a good source–reservoir rock configuration. However, the specific hydrocarbon accumulation conditions of the key blocks and key risk exploration fields remain controversial, and the previous understanding can no longer meet the requirement of risk exploration (Hou et al., 2020). The deep carbonate rocks have undergone multi-stage transformation, and it is difficult to accurately determine the reservoir formation process by relying on the traditional oil and gas reservoir formation research methods and technologies. Previous research shows that the effective combination of various elements, such as the source rock, reservoir rock, cap rock, migration pathway, and trap, is the key factor to hydrocarbon accumulation (Zhao et al., 2006; Zhang et al., 2011a; Li J et al., 2022; Richardson et al., 2022). In this paper, the formation period of carbonate reservoirs in the study area is precisely determined by laser in situ U–Pb isotope dating technology. This research discusses the key stage and model of hydrocarbon accumulation of the Ordovician reservoir in the Gucheng area, from perspectives of source rock conditions, hydrocarbon migration pathways, formation mechanisms of reservoir rocks, and modification of tectonic thermal events. Also, the favorable exploration zones are evaluated according to lessons learned from failure wells and exploration practice. The aforementioned research results are expected to provide more reliable references for ultra-deep hydrocarbon exploration in the Tarim Basin and similar areas.
2 Geological setting
The Gucheng area is located in the east of the Tazhong uplift and southwestward of the Shunnan slope and northward of the Lunnan area. It connects with the Manjiaer sag and Tadong uplift. It is cut by the Cheerchen fault belt in the south (Figure 1A). In terms of geotectonics, the Gucheng lower uplift lies in the transition between the Tazhong and Tadong uplifts. It was formed during the middle Caledonian orogeny and finalized during the late Caledonian orogeny. Subsequently, it was further uplifted due to the Hercynian Northward compression and yet remained tectonically stable during the Indosinian–Himalayan movement (Dai et al., 1996; He et al., 2005; Gao, 2019).
FIGURE 1. Geological setting of the Gucheng area. (A). Structural location of the Gucheng area in Tarim Basin; (B). Comprehensive stratigraphic column of the Ordovician.
A relatively complete stratigraphic association of the Sinian–Ordovician carbonate rocks develops in the Gucheng area, which is most of the carbonate platform and slope-basin deposition (Cai et al., 2013; Huang et al., 2013). The Cambrian–Ordovician in the study area presents an overall paleo-geographic framework characterized by a “platform in west and basin in east.” In other words, the western part is the carbonate platform deposition, while the eastern part is the deposition of the platform margin and basin environments. The platform deposition is associated with a shallow water depth and development of the mound and shoal of the platform margin and the intra-platform grain shoal, of which the scales are controlled by the type and evolution of the platform. Moreover, the slope–basin deposition is found with a predominance of muddy sediments and considered favorable for development of high-quality source rocks (Figure 1B).
3 Samples and methods
The samples of this research are all collected from the 18 prospecting wells penetrating the Ordovician carbonate rock in the Gucheng area, Tarim Basin (Figure 1A). The conventional way to determine the relative sequence of diagenetic processes in research is mainly based on the contact relationships of minerals of varying stages revealed by the features observed in core observation and thin-section microscopy. The absolute age of minerals of a given stage can also be measured using the solution-based U–Pb isotope geochronometry (Woodhead et al., 2006; Woodhead and Pickering, 2012; Yuan et al., 2022). Nonetheless, these methods have the following disadvantages: first, the method based on the contact relationship among minerals of varying stages can only determine the relative sequence of diagenetic processes of a given sample, and in other words, it cannot directly determine the formation sequence of the same mineral component in different samples. Second, the solution-based U–Pb dating demands that samples to be tested have a sufficient content of U and Pb and consumes a large quantity of samples. However, the ancient marine carbonate rock is commonly associated with low content of U and Pb (Pickering et al., 2010) and small diameters of diagenetic components, resulting in failure to provide enough samples for tests (Hu et al., 2020; Li 2022), which restrains the application of the method. Over the past few years, these problems are all solved by the extensive application of laser ablation (LA)-based in situ U–Pb dating (Li Y. L et al., 2014; Coogan et al., 2016; Roberts et al., 2017; Roberts et al., 2020). After importing and digesting the foreign advanced technology, the CNPC Key Laboratory of Carbonate Reservoirs develops the LA-based in situ U–Pb dating specific to low U-content carbonate minerals. The test instrument is the LA-ICP-MS (Element XR), the reference materials are WC-1 (Roberts et al., 2017) and AHX-1 (Shen et al., 2019), and the isotope correction reference material is NIST 614 (Norman et al., 1996). The laser beam diameter is 100 μm, and the ablation frequency is 10 Hz. The main test procedure is presented below: (1) Prepare the sample target. (2) Determine the test zone according to the status of the target component (the LA target is marked in red. (3) Perform the LA and mass spectrometry across the test zone point by point. (4) Process the acquired test data and develop the Concordia diagram. This research targets the Ordovician of the Gucheng area in eastern Tarim and clarifies the key diagenetic stages via the comprehensive analysis based on the LA in situ U–Pb geochronometry assisted by the thin-section petrographic analysis and laser elemental surface scanning to provide references for studying the heterogeneity of the Ordovician reservoirs in the Tarim Basin.
To illustrate the 3D distribution of pore-throats of the reservoir, the micro-nano-scale refined description is performed to produce the 3D pore-throat distribution model, using the high-precision micro-nano CT 3D imaging technology and e-core software for digital cores. The statistics of the parameters such as the pore-throat radius, shape factor, and spatial connectivity are obtained for pore-throat characterization.
The thin-section, cathode luminescence, and inclusion tests are finished in the CNPC Key Laboratory of Carbonate Reservoirs, and for the test methods, please refer to Pan et al. (2016).
4 Results and discussion
4.1 Source rocks
The facies of the slope-basin in eastern Tarim is the main distribution area of sources rocks in the Tarim Basin. In particular, it is claimed that the Gucheng area of eastern Tarim mainly develops the Cambrian Yuertusi Formation, Cambrian Moheershan Formation, and Mid-Lower Ordovician Heituwa Formation, three sets of effective source rocks, which mostly spread over the slope–basin facies belt of the eastern Gucheng uplift, eastern Tarim, after numerous studies reviewed the development of sources on the periphery of the Gucheng area in accordance with the field outcrops and newly acquired drilling and seismic data (Zhu et al., 2016; Guan et al., 2019).
The Terreneuvian source rock of the Cambrian mainly occurs in the Yuertusi Formation of the platform facies belt in the west and the Xidashan–Xishanbulake Formations of the basin facies belt in the east. Zhu et al. (2016); Li et al. (2020) performed geochemical analysis of over 10 outcrops of the Cambrian Yuertusi Formation in the Aksu area, and the black shale of the Yuertusi Formation presents TOC height up to 4%–16%, the highest among the discovered marine source rocks in China. Well Luntan-1 reveals that the black mudstone of the Cambrian Yuertusi Formation is 18 m thick, with TOC of 2.43%–18.48% (averaging 10.1%) and Ro of 1.5%–1.8%, and is considered a high-quality source rock (Yang et al., 2020). Wells TD1 and TD2 in the basin facies belt in the east also reveal this highly over-mature source rock, similar to that in the platform facies belt. The Miaolingian source rock of Cambrian mainly develops in the Moheershan Formation of the platform margin slope–basin facies belt in eastern Tarim, which is encountered in Wells TD2 and TD1 in the basin facies belt. It presents TOC of .51%–2.58% (averaging 1.60%) and Ro of 2.54% and is considered a medium–relatively high-quality source rock. The Mid-Lower Ordovician source rock is concentrated in the Heituwa Formation of eastern Tarim. It is the black shale of the basin facies deposition, with TOC of .50%–1.64% and Ro of 1.16%–2.10%, and represents a medium–highly mature medium–high-quality source rock (Cao et al., 2019).
The analysis of the burial-thermal maturation history (Figure 2) shows that this source rock reaches the peak hydrocarbon generation and expulsion during the middle Caledonian stage. Massive gas generation via oil cracking of paleo-oil reservoirs occurs in the late Caledonian and late Hercynian stages. A large quantity of over-mature gas is generated during the Indosinian–Himalayan stage (Zhang et al., 2011a; Zhang et al., 2011b), which results in sufficient hydrocarbon supply of the Ordovician in the Gucheng area, Tarim Basin. The statistical overview of the source rock parameters is shown in Table 1.
FIGURE 2. History of burial–thermal maturation of a typical well in Gucheng area.
TABLE 1. Source rock parameters.
4.2 Effective migration pathways
As for pathways for hydrocarbon migration, the network pathway system composed of vertical fault systems and lateral unconformities is found with extensive development across the paleo-uplift area, which serves as a good migration channel and effective pathway system of hydrocarbon migration and accumulation (Figure 3) (Mahmud et al., 2020; Shan et al., 2021). On one hand, multiple regional karst unconformities occur at the tops of the Yijianfang, Yingshan, and Penglaiba Formations and Furongian of Cambrian. Moreover, the effective reservoir thickness is large, and the lateral spreading of the reservoir rock is broadened and continuous. These are all in favor of hydrocarbons migrating along unconformities toward the higher position of the flank and accumulating in place. On the other hand, the Gucheng area is found with the development of multiple high-angle tensile normal faults penetrating downward the Cambrian source rock and yet not cutting the overlying regional cap rocks (the Tumuxiuke Formation marlstone and the Queerqueke Formation mudstone). They provide effective vertical channels for hydrocarbon migration from the Cambrian source rock, while maintaining the integrity of the lithological–structural composite trap. Such faults are key factors for hydrocarbon accumulation in the Ordovician in the Gucheng area. In addition, due to invasion of igneous rocks, the paleo-oil reservoirs are baked and destructed, and yet such effects are lower down as further away from the invaded igneous rock (Figure 3). Tumuxiuke Fm is abbreviated as O3t, Yijianfang Fm is abbreviated as O2y, Yingshan Fm is abbreviated as O1+2y, and Penglaiba Fm is abbreviated as O1P. They all belong to the Ordovician.
FIGURE 3. Pathway system composed of vertical faults and lateral unconformities in the Gucheng area. (Section location, AA′, is shown in Figure 1A).
4.3 Adjustment and modification of hydrocarbon accumulation by tectonic thermal events
The slope of the Gucheng area, Tarim Basin, lies at the east end of the Tazhong paleo-uplift, and the paleo-uplift background was established in the early Caledonian period. The southern part of this structural belt is relatively close to the Cheerchen fault, which is highly active during the late Caledonian stage and the late Permian, associated with massive invasion of igneous rocks (Ran et al., 2008; Liu et al., 2010; Zhang et al., 2014). Such Permian massive magmatic invasion alters the geothermal field at that time (raised geothermal thermal gradients), and accordingly, the immature source rock on the periphery of the depression reaches the oil generation threshold, which promotes the hydrocarbon generation rate and quantity and accelerates the evolution of the source rock of the basin. As for the mature source rock in the basin, it is converted into over-mature source rock and enters the depletion stage of hydrocarbon generation (Ran et al., 2008; Liu et al., 2010; Zhang et al., 2014). The adjustment and modification of oil and gas reservoirs attributed to tectonic thermal events have critical influences on the formation and evolution of oil and gas reservoirs in terms of both materials and energy and complicate the hydrocarbon accumulation in the Ordovician of the Gucheng area.
4.3.1 Evidence from the laser in situ U–Pb dating
The Ordovician dolomite reservoir in the Gucheng area, Tarim Basin, has gone through superimposed modification of diagenetic fluids of multiple stages during its formation, which results in the high heterogeneity of the reservoir. To clarify the relative sequence of diagenetic processes of varying stages during the pore evolution of the Ordovician dolomite reservoir and their coupling relationships with pores of the reservoir, precisely determining the stages of the key diagenetic processes is critical. This research, based on the laser in situ U–Pb dating and laser in situ elemental surface scanning and imaging, performs a systematic isotope dating analysis for the three major textural constituents, the surrounding rock matrix, medium–coarse dolomite on the wall of the pore-vug, and calcite cement inside the pore-vug. The test results are shown in Table 2; Figure 4.
TABLE 2. Components of tested samples and results of the laser in situ U–Pb dating.
FIGURE 4. Characteristics of the Ordovician carbonate rock samples of the Tarim Basin (with marked sampling positions), and the U–Pb Concordia diagram. (A). Two textural constituents of the ample tested in DQ17: ① the intergrowth-crystalline calcite in the pore-vug and ② the fine dolomite of the surrounding rock; (B). Sampling positions for the thin section of sample DQ17: ① the intergrowth-crystalline calcite in the pore-vug and ② the fine dolomite of the surrounding rock; (C). U–Pb isotope dating of the intergrowth-crystalline calcite in Sample DQ17; (D). U–Pb isotope dating of the surrounding rock fine dolomite in Sample DQ17; (E). Two tested textural constituents of Sample DQ11: ③ the coarse dolomite in the pore-vug and ④ the fine–medium dolomite in the surrounding rock; (F). U–Pb isotope dating of the surrounding rock fine dolomite in Sample DQ11.
The fine dolomite of the surrounding rock and intergrowth-crystalline calcite in Sample DQ17 are tested (Figures 4A, B). The fine dolomite of the surrounding rock is dated to be 474.7 ± 7.5 Ma (Figure 4C), corresponding to the age of the Ordovician Yingshan Formation in the study area. The intergrowth-crystalline calcite is dated back to 469 ± 22 Ma (Figure 4D), which suggests that the Ordovician is subjected to the stage of calcium-rich hydrothermal fluids during the Caledonian orogeny and pore-vugs are filled with calcite. The fine–medium dolomite of the surrounding rock and the coarse dolomite in the pore-vug in Sample DQ11 are tested (Figure 4E). Owing to the extremely low content of uranium in the coarse dolomite of the fracture-vug, the laser in situ U-Pb dating fails. The fine–medium dolomite of the dark gray surrounding rock formed 346 ± 38 Ma (Figure 4F), indicating a stage of magnesium-rich hydrothermal fluids during the early Hercynian stage, with fractures and vugs filled by coarse calcite (Figures 5A–D), with high positive anomalies of the elements Y and Ce (Figures 5E, F). The filling of the coarse dolomite occurs after the formation of the fine–medium dolomite of the dark gray surrounding rock, which implies that the invasion of hydrothermal fluids migrates along the early Hercynian fault and the filling of coarse dolomite shall be slightly later than 346 Ma. The laser in situ U–Pb dating and the in situ elemental surface scanning and imaging show that the multi-stage tectonic thermal events during the Caledonian and Hercynian movement have essential adjustment and modification effects on deep hydrocarbon accumulation, accompanied by filling with saddle dolomite and calcite.
FIGURE 5. Element surface scanning images of Sample DQ11 in the Tarim Basin. (A). Concentration of 25Mg in horizontal distribution; (B) concentration of 43Ca in horizontal distribution; (C) concentration of 55Mn in horizontal distribution; (D) concentration of 238U in horizontal distribution; (E) concentration of 89Y in horizontal distribution; (F) concentration of 140Ce in horizontal distribution.
4.3.2 Evidence from the reservoir bitumen distribution and genesis
The drilling and core of wells in the study area reveal that from the Yijianfang Formation to the Upper Yingshan Formation and in the Penglaiba Formation occurs the over 1,000-m-thick bitumen paleo-oil reservoir. The reservoir bitumen extensively develops in the dissolution pore-vug (Figure 6A), stylolite and structural fracture (Figure 6B), inter-crystalline (dissolution) pore (Figure 6C), and mold (visceral foramen) pore (Figure 6D) of the Ordovician carbonate reservoir of the paleo-uplift, and presents itself in filling forms of strips, grains, veins, and blocks (Li et al., 2019; Li et al., 2021a; Hou et al., 2020; Qie et al., 2021).
FIGURE 6. Occurrence of bitumen and siliceous hydrothermal metasomatism in the Ordovician carbonate reservoir in the Gucheng area. (A). Bitumen in the dissolution pore-vug, Well GC4, Penglaiba Formation, 6,509 m; (B). bitumen in the stylolite and structural fracture, with vesicles occurring on the bitumen surface, Well GC4, Yijianfang Formation, 5,597–5,600 m; (C) bitumen in the intercrystalline pore of dolomite, Well GC9, Yingshan Formation, 6,097.8 m; (D) bitumen in the mold pore, Well GC7, Yijianfang Formation, 5,662 m; (E) siliceous hydrothermal filling, Well GC15, Yingshan Formation, 6,356.7 m; (F) siliceous hydrothermal filling, Well GC14, Yingshan Formation, 6652 m.
There have been many important understandings provided by previous studies on reservoir bitumen genesis. From the perspective of the genesis, the reservoir bitumen can be divided into three categories: pyrobitumen, biodegraded bitumen, and precipitated asphalt (Zhao et al., 2007). There are significant differences in morphology and maturity of bitumen of different geneses. Due to the high temperature and high pressure, the edge of the pyrobitumen is clearer, while the biodegraded bitumen and precipitated asphalt are often dispersed with blur edges and irregular shapes (Jacob, 1989). In addition, the reflectance of the pyrobitumen derived from crude oil cracking is much higher than those of precipitated asphalt and biodegraded bitumen (Hwang et al., 1998; Gao and Hu, 2002). The reflectance of pyrobitumen is generally above 4.0%–6.0%, and that of precipitated bitumen is usually .5%–1.5% (Ran et al., 2008).
The occurrence and reflectance of the reservoir’s solid bitumen in the Gucheng area show that the solid bitumen is the pyrobitumen produced via the large-scale oil cracking of the original reservoirs affected by magmatic hydrothermal activities. Regardless of dolomite or limestone, the contained bitumen presents clear and straight edges, shapes of regular polygons, and vesicles developed on bitumen surfaces, which are typical features of pyrobitumen and indicate that the paleo-oil reservoir has experienced high-temperature baking. The solid bitumen reflectance is high, from 3.94%–7.75%. The measured reflectance of the same sample is highly variable and the bitumen is highly anisotropic, which implies intensive high thermal maturation. During the process of hydrothermal fluids flowing along faults and fractures, some special minerals, such as quartz, pyrite, fluorite, and bitumen (mainly pyrobitumen), precipitated, due to variation of pressure and temperature and interaction with surrounding rocks (Jin et al., 2006; Chen, 2008). In addition, the development of the siliceous hydrothermal filling also reflects the intensity of hydrothermal alteration (Figures 6E, F).
4.3.3 Evidence from homogenization temperatures of fluid inclusions
Fluid inclusions of the Ordovician reservoir rock in the Gucheng area mainly occur in the calcite vein, granular calcite, and crystalline quartz overgrowth and formed in the middle and late diagenesis. Observation identifies five types of fluid inclusions, namely, solid bitumen inclusion, hydrocarbon-containing brine inclusion, two-phase brine inclusion, gas–liquid two-phase inclusion, and gaseous hydrocarbon inclusion. The bitumen inclusion is derived from the oil inclusion. Heavy hydrocarbons crack due to higher temperatures, and the inside pressure is raised to trigger bursting. Light hydrocarbons escape from the inclusion, and bitumen is left to form the bitumen inclusion, which is a direct evidence of oil emplacement. Gaseous hydrocarbon inclusions and gas–liquid two-phase inclusions may be derived from trapped cracking gas via oil cracking and also later charging of natural gas.
Identification and microthermometry have been performed for the hydrocarbon inclusions and associated brine inclusions in the Gucheng area (Table 3). The homogenization temperature of the organic fluid inclusion typically stands for the lowest temperature at the time the inclusion is captured. In other words, the temperature of the hydrocarbons migrates into the reservoir. Therefore, the peak temperature is indicative of the peak hydrocarbon migration. The analysis of oil stability of the marine facies reservoir in the platform-basin area of the Tarim Basin shows that 150°C is the threshold of crude oil cracking, and massive cracking is anticipated with a temperature over 200°C (Zhao et al., 2001), far higher than the formation temperature in cases of normal geothermal gradients. This suggests that the fluid temperature of the precipitated calcite vein is higher than the temperature of the surrounding rock, and thus such fluids are typical deep hydrothermal fluids. Some geologists (Cai et al., 2008; Li K. K et al., 2010; Zhu et al., 2013) also validate the presence of hydrothermal fluids in the Lower Paleozoic of the Tarim Basin, according to the fact that the formation temperature of calcite is higher than the burial temperature.
TABLE 3. Homogenization temperatures of brine inclusions in minerals filling the fracture-vug of the Ordovician of the Gucheng area, Tarim Basin. Liquid hydrocarbon inclusion is abbreviated as LHI. Solid bitumen inclusion is abbreviated as SBI. Gas–liquid two-phase inclusion is abbreviated as GLI. Gaseous hydrocarbon inclusion is abbreviated as GHI. Brine inclusion is abbreviated as BI.
4.3.4 Effective of paleo tectonic-fluid is a critical factor controlling the formation of hydrocarbon accumulation
The deep carbonate rock has gone through multi-stage variation of fluid-diagenetic environments of the tectonic, thermal, pressure, and fluid regimes and time. The diagenesis is complicated, the diagenetic modification of multiple stages is superimposed, and the reservoir presents high heterogeneity (Chen et al., 2007; Zhao et al., 2012; Wang T. G et al., 2014; Li J et al., 2022). The temperature–pressure fields and fluid types are varied in different tectonic–burial–thermal maturation stages (Huang and Hou, 2001; Li Z et al., 2010; Fan et al., 2020; Li et al., 2021b). The Ordovician reservoir rock in the Gucheng area can be divided into two types, the Ordovician karst-dolomitization reservoir and the karst reef flat reservoir. In this research, the Ordovician karst-dolomitization reservoir is taken as an example to investigate the formation mechanisms of the complicated reservoir, such as the paleo-uplift setting, sedimentary facies, penecontemporaneous dissolution, and tectonic thermal events.
The Lower Ordovician karst-dolomitization reservoir in the Gucheng area, Tarim Basin, mainly occurs in the inner dolomitized shoal of the shallow-water ramp platform of the Lower Yingshan Formation and Penglaiba Formation. The reservoir space is dominated by residual pores, dissolution pore-vugs (Figure 7A), inter-crystalline or inter-granular (dissolution) pores (Figures 7B, C), and fractures. The reservoir samples mostly present medium–low porosity with medium–narrow throats, with high connectivity in local areas. The reservoir rocks are divided into the pore-vug type and fracture-vug type.
FIGURE 7. Reservoir space types and characteristics of the Ordovician karst-dolomitization reservoir in the Gucheng area, Tarim Basin. (A) Gray medium–coarse dolomite with dissolution pore-vugs (intergranular pore), Well GC13, the Yingshan Formation, 6,268 m; (B) medium–coarse dolomite with intercrystalline pores filled with bitumen, Well GC13, the Yingshan Formation, 6,268 m; (C) coarse dolomite with intercrystalline dissolution pores, Well GC9, the Yingshan Formation, 6,095.50 m; (D) pore-throat network model (with resolution of .9 um) with red representing pores and white representing throats, Well GC8, the Lower Yingshan Formation, 6,074.0 m; (E) medium–coarse dolomite with brown luminescence under the cathode ray and some crystals with red rims, Well GC14, the Yingshan Formation, 6,237.2 m; (F) medium–coarse dolomite with calcite hydrothermal filling, Well GC14, the Yingshan Formation, 6,237.2 m.
The CT comprehensive characterization of the Ordovician dolomite reservoir is shown in Figure 7D. CT scans of the reservoir pores show that the reservoir of the dolomitized shoal has higher micro-heterogeneity, manifested as the skewed distribution of pore-throats (uneven pore-vug diameter distribution from .2 mm–10 mm), medium-narrow throats, a lower quantity of throats with uneven distribution of radii, and higher connectivity in local areas.
The development of the karst-dolomitization reservoir of the Lower Yingshan Formation and Penglaiba Formation is controlled by the paleo-uplift and sedimentary facies settings in the early stage. Moreover, the reservoir is subjected to the superimposed modification of the penecontemporaneous karstification, shallow burial dolomitization, and late faulting–hydrothermal activity. After a comprehensive analysis, it is claimed that the inner grain shoal of the shallow-water ramp serves as the basis for development of the dolomite reservoir, while the penecontemporaneous exposure dissolution is key to the formation of the reservoir. Pores are mostly inherited from the previous dolomitized shoal, while the faulting–hydrothermal modification creates important extra pores. (1) The shoal facies is the basis of the development of the dolomitized shoal reservoir, and the distribution of high-quality reservoirs is closely related to the inner dolomitized shoal of the shallow-water ramp. The reservoir dominated by the matrix pore-vug is mostly found in the fine–medium dolomite, which presents the phantom granular texture and along-bedding development of pores. This suggests that the dolomitized shoal is the basis for large-scale development of the reservoir, and the reservoir is a typical shoal-controlled reservoir. In addition, according to the analysis of the residual or restored original rock texture, the original rock of the crystalline dolomite is mostly grainstone of the shoal facies. The inter-granular (crystalline) pores of the dolomitized shoal deposition are the main reservoir space, and the sparry grainstone and wackestone are tight with fewer pores. (2) The penecontemporaneous exposure dissolution is key to the formation of pores. The systematic coring over 100 m in Well GC601 reveals that the cored interval has over 30 exposure karst surfaces associated with extensive geopetal textures and vadose silt zones. The pore-vug interval mainly occurs in the dolomitized shoal below the top exposure surface of the high-frequency cycle, representing a typical penecontemporaneous fabric-selective dissolution and providing flow channels for dolomitization fluids in the later shallow-burial stage. (3) The dolomite reservoir mainly presents itself along the permeable shoal, fault, and unconformity surface. Pores are mostly the previous pores that are inherited and preserved. The samples are generally seen with brown luminescence under the cathode ray, and some crystals present bright red rims (Figure 7E), which indicates that the dolomite of the study area is mainly the burial metasomatism genesis, with late hydrothermal modification in local areas. The hydrothermal fluids derived from deeper layers serve as the diagenetic media for the saddle dolomite. From the perspective of the dissolution–precipitation of minerals with material balance and varying temperature and pressure conditions, the dissolution and cementation are in unity of opposites. The end of the tectonic hydrothermal activity is often associated with fillings of siliceous hydrothermal fluids, saddle dolomite, and calcite (Figure 7F) (Jiao et al., 2011; Chen et al., 2012).
4.4 Hydrocarbon accumulation model and predicted favorable zones of the Ordovician in the Gucheng area, Tarim Basin
4.4.1 Hydrocarbon accumulation model
The overall paleo-geographic framework of the Ordovician in the Gucheng area, Tarim Basin, features the transition from the platform environment to the basin environment. The Ordovician is close to the main source rock, and the hydrocarbon generation and accumulation are characterized by the generation in the basin and storage in the platform. According to the staged basin structural evolution, burial–thermal maturation simulation, and analysis of the main control factors of hydrocarbon accumulation, the hydrocarbon accumulation of the ancient deep carbonate reservoir can be divided into three stages (Figure 8).
FIGURE 8. Hydrocarbon accumulation and evolution model in Gucheng area, Tarim Basin. (A) Formation of the primary oil and gas reservoir. The hydrocarbon generation of the three source rocks in the Cambrian–Ordovician of the Tarim Basin lasts until the late Hercynian stage, during which the primary oil reservoirs are formed, mostly in carbonate rock traps with some in the Silurian clastic rock. (B) Destruction and cracking of the primary oil reservoir. Due to the magmatic hydrothermal activities of multi-stage tectonic thermal events during the Caledonian and Hercynian stages, the primary oil reservoirs are subjected to oil cracking and the cracking gas reservoirs and residual paleo-oil reservoirs (or bitumen) are formed. (C) Adjustment, destruction, and reforming of gas reservoirs. The study area is tectonically stable after the Triassic. The trap integrity is maintained, and the preservation condition is good. The Cambrian–Ordovician source rock in the Manjiaer depression enters the hydrocarbon generation depletion stage, and part of crude oil is converted into natural gas via cracking, which forms condensate reservoirs. The dispersed residual organic matter in the source starts to generate gas at a large scale and forms the Himalayan gas reservoir, mostly occurring in traps related to the Himalayan movement.
4.4.2 Prediction of favorable zones
Crude oil cracking of paleo-oil reservoirs to generate gas is an important way to form deep natural gas, and such cracking gas is the main target for natural gas exploration of highly over-mature marine carbonate reservoirs in China (Zhao et al., 2007; Wang et al., 2008; Song et al., 2021; Wang and Wang, 2021). The analysis of the main controlling factors of the hydrocarbon accumulation in the Gucheng area, Tarim Basin, and the corresponding hydrocarbon accumulation evolution model suggest that the crude oil of the paleo-oil reservoir is massively converted into pyrobitumen and natural gas. The phase transition of deep fluids results in more rigorous requirements of hydrocarbon accumulation. With respect to the hydrocarbon exploration of the Ordovician in the Gucheng area, Tarim Basin, the following principle is recommended. The Caledonian–Early Hercynian primary oil reservoir shall be searched in the upper Ordovician karst reef flat reservoir on the periphery of the depression, far away from igneous rock invasion. The Late Hercynian cracking gas reservoir shall mostly occur in the Lower Ordovician karst-dolomitization reservoir along the paleo-oil reservoir and depression periphery. The exploration of the Himalayan gas reservoir shall focus on the large-scale gas generation of the liquid hydrocarbon scattered within the source rock during the highly over-mature stage. In summary, the western and northern parts of the paleo-uplift, with the premium source–reservoir–cap rock assemblage and fewer effects of faulting and tectonic hydrothermal activities, are the favorable exploration zones of hydrocarbon migration and accumulation.
5 Conclusion
1) The Ordovician oil and gas reservoir in the study area is attributed to the oil-cracking gas and late natural gas charging. The main controlling factors of the hydrocarbon accumulation in the Ordovician of the Gucheng area are the favorable paleo-structural setting, effective development of source rock, effective pathway system, modification of tectonic thermal events to hydrocarbon accumulation, and development conditions for high-quality reservoir rocks.
2) The paleo-tectonic-fluid effect is an important factor controlling the development of the reservoir rock and natural gas accumulation. The Ordovician karst-dolomitization reservoir is taken as an example to investigate the superimposed modification of various mechanisms, such as the paleo-uplift setting, sedimentary facies belt, penecontemporaneous dissolution, and tectonic thermal event. The grain shoal is the basis for the development of the dolomite reservoir, while the penecontemporaneous exposure dissolution is the key factor for reservoir formation. Pores are mostly inherited from the previous dolomitized shoal deposit, and faulting–hydrothermal modification creates important extra pores.
3) The formation and evolution of the Ordovician oil and gas reservoir in the Gucheng area, Tarim Basin, can be divided into three stages: the formation of primary oil and gas reservoirs, oil-cracking gas reservoirs, and adjustment, destruction, and reforming of gas reservoirs. The hydrocarbon accumulation model has the characteristics of multi-stage evolution.
4) Deep hydrothermal fluids migrate upward via faults, which is manifested as both destruction of the fault and vug-fracture reservoir system and constructive dissolution in different areas. The distribution mechanism for dissolution expansion and cementation still needs further investigation. Given the major challenge of poor continuity of high-quality reservoir and reservoir heterogeneity, it is recommended to quantitatively analyze the mechanisms of formation and preservation (dissolution and precipitation) of pores in the reservoir during the paleo–tectonic–hydrothermal process so as to reveal the distribution pattern and scale of high-quality reservoir rocks. In addition, given the small impedance difference between the low-porosity, low-permeability dolomite reservoir and tight limestone, it is suggested to enhance the seismic prediction technology for high-quality reservoirs, with the geological background of the study area taken into consideration. The future exploration practice shall target the northern and western parts of the Gucheng uplift that has a good source–reservoir–cap rock assemblage and is less affected by faulting and magmatic invasion.
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
YZ, YN, and QL contributed in writing, reviewing, and editing; data curation; and writing—original draft preparation; BL, YS, and YP contributed in formal analysis, validation, and reviewing.
Funding
This study was supported by the National Science and Technology Major Project (No. 2016ZX05004-002).
Acknowledgments
We thank all editors and reviewers for their helpful comments and suggestions.
Conflict of interest
Author YN was employed by PetroChina Daqing Oilfield Company.
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
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Keywords: key accumulation stage, laser in situ U–Pb dating, hydrocarbon accumulation, Ordovician, Gucheng area
Citation: Zhang Y, Li Q, Niu Y, Li B, Shi Y and Pang Y (2023) Key stage and model of hydrocarbon accumulation of Ordovician reservoir in Gucheng area, Tarim Basin, China. Front. Earth Sci. 10:1108734. doi: 10.3389/feart.2022.1108734
Received: 26 November 2022; Accepted: 28 December 2022;
Published: 12 January 2023.
Edited by:
Hu Li, Southwest Petroleum University, ChinaReviewed by:
Xixin Wang, Yangtze University, ChinaYunfeng Zhang, Southwest Petroleum University, China
Xiujian Ding, China University of Petroleum, China
Copyright © 2023 Zhang, Li, Niu, Li, Shi and Pang. 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: You Zhang, zhangshiyouda@126.com