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Abstract

The Lower Permian Shanxi Formation marine–continental transitional organic-rich shale is one of the most important potential shale gas plays in the Ordos Basin, China. However, the content and origin of desorbed gas from the Shanxi Formation are poorly documented, limiting the understanding of gas generation and potential play elements. Geochemical characteristics of desorbed gas, including content and origin, are analyzed from 17 core samples of the Shanxi Formation from well SL-1. The results show that the Shanxi Formation shales in the study area are characterized by high total organic carbon content of 1.17–2.63%, type III organic matter, and high T_max between 493 and 513℃. The desorbed gas content of the shale samples varies from 0.22 to 0.50 m³/t, with an average of 0.37 m³/t, and shows a positive correlation with total organic carbon. The gases are dominated by methane (69.57–89.02%), with small amounts of ethane (0.01–0.09%). The carbon isotopic signature δ¹³C₁ ranges from −49.5 to −45.3‰, and the δ¹³C₂ ranges from −23.3 to −14.7‰. In addition, gases released from the Shanxi Formation core samples are thermogenic in origin and possibly coal derived, as the Whiticar chart and the diagram of ethane versus δ¹³C₂ suggest.

Keywords

Marine–continental transitional shale desorbed gas gas origin Shanxi Formation Ordos Basin

Introduction

Organic-rich shales are potentially significant unconventional hydrocarbon resources and have received remarkable attention in the past few years (Hill et al., 2007; Strapoc et al., 2010; Wang et al., 2015; Zhang et al., 2012). Shale gas is derived from the biodegradation and/or the thermal maturation of retained organic matter, and stored in shale reservoirs mainly as free gas in fractures and pores, adsorbed gas on the surface of inorganic minerals and in organic matter, and slightly dissolved gas in oil and water (Jarvie et al., 2007; Strapoc et al., 2010; Zhang et al., 2012). Unlike conventional natural gas resources, which are buoyancy-driven discrete accumulations in stratigraphic or structural traps (Law and Curtis, 2002), the shale gas is generated and stored in a low-porosity and low-permeability shale, which acts as both the source rock and reservoir rock (Hill et al., 2007). With the development of horizontal drilling and hydraulic fracturing, shale gas exploration has achieved remarkable success in the United States, which fueled high enthusiasm for investigation into the potential of shale gas worldwide (Jarvie et al., 2007).

In contrast to the United States, where shales were deposited in foreland marine settings, China has organic-rich shales from various depositional environments, including marine, marine–continental transitional, and lacustrine (Zou et al., 2010). After nearly 10 years of exploration, gas has been discovered in multiple shale units across China, including the Paleozoic marine shale in the southern Sichuan Basin and the Mesozoic lacustrine shale in the Ganquan Xiasiwan area of the Ordos Basin (Dai et al., 2016). The widely distributed Paleozoic shale in the southern Sichuan Basin was mainly deposited in a deep marine shelf depositional environment and has a thickness of 40–500 m; these Paleozoic marine shales are characterized by high total organic carbon (TOC) (1–8%) and vitrinite reflectance (R_o) (1.3–5%) as well as type I and/or II₁ kerogen (Dai et al., 2016; Jiang et al., 2016). The Chang 7 shale in the Ordos Basin was deposited in a deep to semideep lacustrine environment and has a thickness ranging from 40 to 100 m; Chang 7 lacustrine shale has extremely high TOC (6–14%) and low R_o (mostly less than 1.2%), and the kerogen is type II₁ and/or II₂ (Dai et al., 2016; Wang et al., 2015). Moreover, multiple marine–continental transitional organic-rich shales were deposited from the Carboniferous to Permian, in northern and northwestern China and on the Yangtze Platform, that possess great potentials for shale gas exploration (Jiang et al., 2016). However, the marine–continental transitional black shale is frequently interbedded with coal seams, argillaceous shales, and sandy shales, evidence of the complexity of geological conditions at the time of deposition. Commercial success has not been achieved in the Lower Permian Shanxi Formation (Dang et al., 2016).

The southeastern margin of the Ordos Basin is one of the most important coalbed methane exploration targets in China, and many wells exist in the field (Li et al., 2014). The Lower Permian Shanxi Formation contains organic-rich shale that was deposited in a marine–continental transitional environment. This shale, which is generally interlayered with coalbeds (Li et al., 2016), provides an ideal formation to investigate the properties of shale gas. A series of studies have been carried out on the gas generation, resource potential, and reservoir characterization of marine–continental transitional shale in the southeastern Ordos Basin (Tang et al., 2016; Yan et al., 2015). However, the geochemical characteristics, as well as the origin of the gases in this field, have received little attention and are more poorly understood. Here, we present the geochemical observations (TOC, T_max, chemical composition, and stable carbon isotopes) to describe the content of desorbed gas of the Upper Paleozoic Shanxi Formation shale from core samples of well SL-1 in the Ordos Basin and to provide a more comprehensive understanding of its origin.

Geological setting

The Ordos Basin is located in northern-central China (Figure 1(a)) and is the second largest sedimentary basin in China, with an area of approximately 37 × 10⁴ km². The Ordos Basin contains up to 10 × 10⁸ metric ton of oil in its Mesozoic reservoirs (Duan et al., 2008), and natural gas reserves up to 1789.3 × 10⁹ m³ (Feng et al., 2016). The basin has six major substructures: the Jinxi Fold Belt in the east, the Tianhuan Depression and Western Edge Thrust Belt in the west, the Weibei Uplift in the south, the Yimeng Uplift in the north, and the central Yishan Slope (Figure 1(a)) (Duan et al., 2008).

Figure 1.

(a) Location of the study area and the substructure zones of the Ordos Basin (modified from Duan et al., 2008). (b) Stratigraphic columns and depositional environments of the Ordos Basin (modified from Wang et al., 2015).

The long-lived polycyclic Ordos Basin formed from the middle Proterozoic to the Tertiary; Paleozoic, Mesozoic, and Cenozoic sedimentary strata were developed and preserved in the basin (Figure 1(b)) (Yang et al., 2005, 2016). During the late Early Ordovician, the basin experienced a marine transgression that resulted in the deposition of the Majiagou Formation in the interior of the basin (Yang et al., 2005). The depositional environment was characterized by tidal flats during the Benxi deposition and evolved from the tidal-flat and shallow-marine Taiyuan environments to a fluvial-deltaic environment during the Early Permian Shanxi deposition. The Xiashihezi Formation was deposited onto the Shanxi Formation along with the fluvial sandstones (Gao and Wang, 2017; Guo and Liu, 1999; Li et al., 2016; Yang et al., 2005). The polycyclic fluvial-lacustrine clastic rocks deposited from the late Triassic to Cretaceous in the Ordos Basin formed the Triassic, Jurassic, and Cretaceous Formations (Wang et al., 2015).

The study area is located in the Jinxi Fold Belt (Figure 1(a)) along the southeastern margin of the Ordos Basin. This area experienced multiple tectonic events since the Mesozoic and experienced more tectonic deformation than the internal areas of the Ordos Basin (Wang et al., 2010). In the study area, the main coal-bearing sequences are in the Taiyuan Formation and Shanxi Formation, and the net coal seam thicknesses are 4.49 and 5.73 m, respectively (Ding et al., 2012). The No. 4 and No. 5 coal seams in the Shanxi Formation are the primary sources for coalbed gas development, with a total thickness ranging from 0.5 to 30 m (Chen et al., 2015). Previous work has been performed to determine the geochemical characteristics and origin mechanism of the coalbed methane in this area (Li and Zhang, 2013; Li et al., 2014). In contrast, little attention has been paid to the geochemical characteristics of gases from the lower Permian marine–continental transitional shale associated with these coals. Shales from the Shanxi Formation are widely distributed and have a thickness ranging from 10 to 50 m (Li et al., 2016). The shale lithology includes dark gray and black shale, interbedded with coal and tight sandstone (Yan et al., 2015). Due to its extent and high TOC of 2–7%, the Shanxi Formation shale is one of the main shale gas exploration targets in the Ordos Basin (Jiang et al., 2016; Li et al., 2016).

Sampling and experiments

Sampling

This study used 17 Shanxi Formation core samples from a depth of 1435 to 1476 m from well SL-1 (Figure 1(a)). The lithology of the core samples included gray thinly bedded fine sandstone, coal, and thick black shale (Figure 2). Freshly retrieved cores were immediately placed into a transparent sealed canister filled with saturated salt water and then immersed upside down in water for transportation.

Figure 2.

Petrological characterization and geochemical log of the drilled section of SL-1 well that corresponds to the cored section samples in this study.

Desorption experiments

The desorption experimental setup and gas collection method used in this study follows the procedure described in Wang et al. (2015). Gas samples were collected at temperatures of 20, 60, 80, 90, and 100℃, and then the desorbed gas content was measured. The ambient temperature (20℃) was used to measure the free gas quantity, and 60℃ was the estimated in situ reservoir temperature (assuming that the surface temperature was 20℃ and the geothermal gradient was 30℃/km) used to measure the geochemical character of gases at reservoir conditions. The temperatures of 80, 90, and 100℃ were tested to ensure that the adsorbed gas was completely released. Each temperature test was finished when the released gas fell below 5 ml within a 5 h window.

Gas geochemical analysis

The chemical compositions and stable carbon isotopes of the gas samples were analyzed in the Key Laboratory of Petroleum Resources Research, Institute of Geology and Geophysics, Chinese Academy of Sciences, Lanzhou, China. Chemical compositions were determined using the MAT 271 mass spectrometer, and the concentration of gas was calculated according to the national standards (State Standard of China GB/T 6041-2002 and GB/T 10628-89). Stable carbon isotopes were measured on a Finnigan Mat Delta Plus mass spectrometer interfaced to an HP 5890 II gas chromatograph. Individual hydrocarbon gas components and CO₂ were separated using a fused silica capillary column (PLOTQ 30 m × 0.32 mm) in the gas chromatograph. Stable isotope ratios for carbon are reported in δ-notation in parts per mil (‰) relative to Vienna Pee Dee Belemnite. The measurement precision was estimated to be ±0.5‰ for δ¹³C.

Results and discussion

Geochemical characteristics

Geochemical characteristics of the core samples are listed in Table 1 and Figure 2. The TOC content of the shale is high, ranging from 1.17 to 2.63% with an average of 2.11%; the coal and argillaceous siltstone TOC contents range from 76.00 to 88.50% and 0.91 to 1.76%, respectively (Table 1). As shown in Table 1, the sum of the free and transformed hydrocarbons (S₁ + S₂) for the shale varies from 0.41 to 1.63 mg HC/g rock with an average value of 0.76 mg HC/g rock, which suggests that the Shanxi Formation shale has poor genetic potential.

Table 1.

Geochemical characteristics of the core samples and the chemical composition and stable carbon isotope of desorbed gas.

Sample ID	Depth (m)	Lithology	TOC (%)	S₁ + S₂ (mg/g)	T_max (℃)	δ¹³C_org (‰)	Gas yield (m³/t)	Chemical composition (%)						Stable carbon isotopes (‰)			⁴⁰Ar/³⁶ Ar
Sample ID	Depth (m)	Lithology	TOC (%)	S₁ + S₂ (mg/g)	T_max (℃)	δ¹³C_org (‰)	Gas yield (m³/t)	CH₄	C₂H₆	CO₂	H₂	N₂	Ar	δ¹³C₁	δ¹³C₂	δ¹³C_CO2	⁴⁰Ar/³⁶ Ar
SL1-1	1435.8	Coal	88.50	109.41	481	−24.8	20.36	89.51	0.10	0.57	0.15	9.43	0.23	−41.0	−18.9	−17.0	nd
SL1-2	1438.1	Shale	1.17	0.41	513	−24.3	0.22	81.57	0.03	0.89	0.01	17.15	0.36	−45.4	−14.7	−23.5	nd
SL1-3	1442.6	Shale	1.99	0.60	508	−24.1	0.42	85.93	0.05	0.88	0.23	12.60	0.30	−45.3	−19.8	−23.8	nd
SL1-4	1443.1	Shale	2.31	0.67	506	−24.2	0.50	69.57	0.06	1.69	0.04	28.05	0.60	−47.8	−18.8	−22.8	299.6
SL1-5	1445.5	Argillaceous siltstone	0.91	0.16	506	−23.8	0.13	78.85	0.03	0.25	0.01	20.47	0.40	−47.0	−19.4	−18.5	nd
SL1-6	1450.5	Fine sandstone	nd	nd	nd	nd	0.16	83.72	0.04	1.88	0.07	13.99	0.29	−46.8	−22.4	−24.0	nd
SL1-7	1451.8	Fine sandstone	nd	nd	nd	nd	0.21	69.47	0.04	1.69	0.20	28.01	0.60	−46.9	−25.5	−23.9	301.3
SL1-8	1455.8	Shale	2.27	0.64	514	−23.8	0.42	82.69	0.08	1.56	0.02	15.28	0.37	−45.8	−20.2	−26.6	nd
SL1-9	1457.5	Shale	2.21	0.81	508	−23.6	0.29	87.81	0.06	0.78	0.02	11.06	0.26	−47.2	−20.6	−23.9	nd
SL1-10	1459.0	Shale	1.73	0.73	508	−23.7	0.31	89.02	0.09	0.58	0.03	10.06	0.22	−49.2	−23.3	−21.0	nd
SL1-11	1460.6	Shale	1.75	0.83	493	−23.8	0.37	86.65	0.06	0.50	0.01	12.49	0.30	−47.7	−17.9	−23.0	304.7
SL1-12	1462.2	Shale	2.15	0.62	501	−24.8	0.40	82.47	0.07	1.41	0.01	15.66	0.37	−46.3	−19.0	−21.4	nd
SL1-13	1463.1	Coal	76.00	80.17	487	−23.6	15.39	93.12	0.08	0.72	0.22	5.73	0.14	−46.8	−18.8	−18.2	297.9
SL1-14	1464.0	Shale	2.63	0.49	498	−23.7	0.28	77.48	0.01	0.80	0.01	21.21	0.49	−46.7	nd	−20.9	nd
SL1-15	1468.4	Argillaceous siltstone	1.76	1.17	494	−23.9	0.27	84.10	0.03	0.83	0.02	14.69	0.34	−48.5	−20.9	−27.2	nd
SL1-16	1473.3	Shale	2.44	1.63	499	−23.8	0.46	85.34	0.08	1.77	0.06	12.45	0.30	−48.7	−18.1	−25.1	297.2
SL1-17	1475.1	Shale	2.56	0.98	505	−23.6	0.41	86.06	0.09	1.94	0.14	11.50	0.27	−49.5	−22.1	−17.6	nd

nd: no data; TOC: total organic carbon.

The maximum temperature at the S₂ peak, T_max, ranges from 481 to 513℃. Thus, all samples are above 470℃ and fall in the gas window according to Peters (1986). Previous studies have shown that the average R_o of the Shanxi Formation shale in the eastern Ordos Basin is 1.89% (Lan et al., 2016), indicating a highly matured organic matter. Moreover, all Shanxi Formation shale samples have organic carbon isotopic compositions (δ¹³C_org) ranging from −24.8 to −23.6‰, indicating that they contain type III organic matter according to the evaluation standard presented by Hu and Huang (1991) (Figure 3).

Figure 3.

The organic carbon isotopic compositions (δ¹³C_org) of the core samples.

The content and constraints of desorbed gas

The evaluation of shale gas content is very important for resource potential evaluation and productivity prediction (Strapoc et al., 2010). The desorbed gas content of samples at different temperatures is shown in Figure 4. At ambient temperature (20℃) the amount of gas released was relatively low, except for the coal samples which reached up to 12.91 m³/t; however, the amount of gas released at the reservoir temperature (60℃) was significantly greater. At high desorption temperatures (80, 90, 100℃), the amount of released gas was in equilibrium. The desorbed gas contents of shale samples varied from 0.22 to 0.50 m³/t with an average value of 0.37 m³/t. The average desorbed gas content of coal, fine sandstone, and argillaceous siltstone was 17.88, 0.19, and 0.20 m³/t, respectively.

Figure 4.

Plot of desorbed gas content of fine sandstone, argillaceous siltstone, shale, and coal samples at different desorption temperatures (arrows correspond to the ordinate).

Following previous studies of the Longmaxi Formation marine shale in the Jiaoshiba area (Zhang et al., 2015) and Chang 7 lacustrine shale in the Xiasiwan area (Fan et al., 2017), the desorbed gas content of shales from various depositional environments was compared (Figure 5). As shown in Figure 5, the mean desorbed gas content of the marine–continental transitional shale (0.37 m³/t) is lower than both the marine (0.79 m³/t) and terrestrial (1.29 m³/t) shale, but the desorbed gas content of the Shanxi Formation shale falls in a similar range as the Longmaxi Formation. This indicated that the marine–continental transitional shale of the Shanxi Formation in the Ordos Basin has a potential for shale gas exploration.

Figure 5.

Comparison of desorbed gas content of shales in different depositional environments (marine, Zhang et al., 2015; terrestrial, Fan et al., 2017).

The amount of desorbed gas shows a positive correlation with TOC (Figure 6). Strong correlations between total gas and TOC (R² of approximately 0.7–0.9) were also found from canister desorption of fresh cores from the Devonian–Mississippian New Albany Shale in the Illinois Basin, United States (Strapoc et al., 2010), indicating that the organic matter content is primarily responsible for total gas content in these shale samples. Based on the experiments of high-pressure methane adsorption of the Longmaxi shale samples, Pan et al. (2016) found that the adsorbed gas capacity of the samples positively correlated to TOC. The quantity of organic matter in shales not only determines hydrocarbon generation potential but also creates abundant organic nanopores, which provide more internal surface area and promote shale gas adsorption (Sun et al., 2015).

Figure 6.

Relationship of desorbed gas content with TOC. TOC: total organic carbon.

Origin of nonhydrocarbon gases

Table 1 presents the chemical and stable carbon isotope composition of desorbed gas from the desorption experiments at reservoir temperature (60℃). Gas released from the core samples contained many nonhydrocarbon gases, mainly CO₂ and N₂.

Origin of CO₂

The CO₂ concentration varies from 0.25 to 1.94%, and the δ¹³C of CO₂ ranges from −27.2 to −17.6‰ with an average of −22.9‰ (Table 1). The sources of CO₂ in coals and shales depend on several biogenic and abiogenic processes: oxidation of sedimentary organic matter, microbial and thermogenic alteration of organic matter, thermal decomposition of carbonates, and magmatic or mantle degassing (Imbus et al., 1998; Wycherley et al., 1999). Various studies have been used to evaluate the origin of CO₂ (Kotarba and Rice, 2001).

The correlation of δ¹³C₁ and δ¹³C_CO2 (Figure 7) indicated that CO₂ of desorbed gas was generated mainly during the thermal transformation of organic matter. According to the analysis above, the core samples contain type III organic matter; thus, it is suggested that the CO₂ was produced through catagenesis and metagenesis of the humic or coaly of type III kerogen source rocks.

Origin of N₂

Figure 7.

Genetic characterization of analyzed gases from the Shanxi Formation using δ¹³C₁ versus δ¹³C_CO2. Compositional fields modified after Kotarba and Rice (2001).

N₂ is one of the most common nonhydrocarbon gases found in coalbed methane and shale gas (Burruss and Laughrey, 2010; Flores et al., 2008). Sources of N₂ in natural gas include thermal decomposition of organic matter and high ammonium clays, as well as the deep crust and mantle (Wang, 1990). It can also be derived from the atmosphere or trapped during sedimentation (Krooss et al., 1995).

As shown in Table 1, the N₂ concentration varies from 10.06 to 28.05% with an average of 16.31%, exhibiting a negative correlation with methane (Figure 8). The ratio of N₂/Ar in desorbed gases ranged from 41.3 to 51.2, with an average of 44.4. Furthermore, the ⁴⁰Ar/³⁶Ar ratios of some desorbed gas were also measured (Table 1), which are similar to the atmosphere (295.5) (Allegre et al., 1987) and indicate that the Ar is of atmospheric origin. In addition, previous studies have shown that the atmospheric ratio of N₂/Ar was 83.3, and the ratio of N₂/Ar in gas dissolved in water was 38 (Wang et al., 1994). The ratio of N₂/Ar in desorbed gas is less than the atmospheric ratio (83.3) but higher than the ratio of gases dissolved in water (38); the high N₂ content of the samples suggested the infiltration of surface water and atmospheric-derived N₂ into the strata. In addition, previous studies suggested that the study area underwent complex tectonic deformation from the Mesozoic to Cenozoic (Li and Zhang, 2013; Li et al., 2014), which provided strong hydrodynamic subsurface conditions and led to the high N₂ concentration measured in the core samples.

Figure 8.

N₂ versus methane concentrations of desorbed gas from the Shanxi Formation core samples.

Origin of hydrocarbon gases

The carbon isotope composition of methane and associated gases, in combination with molecular composition, can be used to infer the origin of natural gas (Whiticar, 1999). Biogenic methane has δ¹³C less than −60‰ and thermogenic methane has δ¹³C greater than −55‰ (Whiticar, 1999). As shown in Table 1, the content of methane and ethane varies from 69.47 to 89.02% and from 0.01 to 0.09%, respectively, with respective averages of 82.05 and 0.05%. In this study, methane is the dominant constituent of the desorbed gases. The δ¹³C₁ ranges from −49.5 to −45.3‰ (average −47.3‰), while the δ¹³C₂ ranges from −25.5 to −14.7‰ (average −20.2‰). Due to the relatively dry desorbed gases in this study (C₁/C_1–5 =1.00), the diagram of the hydrocarbon gas component ratio C₁/C₂₊₃ versus δ¹³C₁ is used to better distinguish between biogenic and thermogenic gases (Golding et al., 2013; Whiticar, 1999). Both molecular and isotope compositions (Figure 9) show that the desorbed gases generally relate to a combination of bacterial and thermogenic processes.

Figure 9.

C₁/C₂₊₃ versus δ¹³C₁ for gases from the Shanxi Formation core samples (after Whiticar, 1999).

The desorbed gases from the Shanxi Formation core samples shows relatively light carbon isotopic composition of δ¹³C₁ which is similar to the coalbed methane in the southeastern margin of the Ordos Basin (Figure 9) (Li et al., 2014). Previous studies have shown that the meteoric and surface water might flow into the deeper strata of the Shanxi Formation, influenced by the Liulin Nose Structure (Li et al., 2014). Since ¹³CH₄ is much more easily transported away by water, the strong hydrodynamic conditions could cause the carbon isotopes of coalbed methane to become lighter (Li et al., 2014; Qin et al., 2005, 2006). Thus, the light carbon isotopes of methane and high N₂ content measured in this study might also be related to past complex tectonic movements that created strong hydrodynamic conditions. Therefore, it is believed that the origin of the desorbed gases in the study area is thermogenic and that the strong hydrodynamic conditions depleted the methane of ¹³C.

Thermogenic gases can be classified into oil gases, derived mainly from marine sapropelic organic matter (Type I kerogen), and coal gases derived from humic organic matter (Type III kerogen) (Ni et al., 2013). Previous studies have suggested using the δ¹³C of ethane for distinguishing the origin of thermogenic gases (Dai et al., 2005; Ni et al., 2013). Based on a comprehensive study on the geochemical characteristics of natural gases in the main Chinese basins, a δ¹³C₂ of natural gas less than −28‰ is oil-derived gas, and a δ¹³C₂ greater than −28‰ is coal-derived gas (Wang et al., 2015). As shown in Figure 10, gases in this study are coal-derived gases.

Figure 10.

Plot of δ¹³C₂ versus C₂H₆ of desorbed gases from the Shanxi Formation.

Conclusions

The characteristics and origin of desorbed gas of the Shanxi Formation were analyzed in this paper, and the following conclusions can be drawn:

The desorbed gas content of the Shanxi Formation shale varies from 0.22 to 0.50 m³/t with an average value of 0.37 m³/t, which is lower than the Longmaxi Formation shale (0.79 m³/t) and Chang 7 shale (1.29 m³/t). The marine–continental transitional shale of the Shanxi Formation in the Ordos Basin has gas exploration potential.

Stable carbon isotopic data and molecular composition of the desorbed gas show that it is thermogenic in origin. Based on the δ¹³C of ethane, the desorbed gas derives from Type III (humic) kerogen sources. However, the strong hydrodynamic conditions in the study area depleted the methane of ¹³C.

δ¹³C_CO2 and organic matter type of the core samples suggest that the CO₂ was produced through catagenesis and metagenesis of humic or coaly type III kerogen. The ratios of N₂/Ar and ⁴⁰Ar/³⁶Ar indicate that the high N₂ content of the core samples may originate from the atmosphere, by infiltration of surface water into the strata.

Footnotes

Acknowledgments

We would like to acknowledge Professor Xianbin Wang and Professor Liwu Li from Analytical Service Center, Research Center for Oil and Gas Resources, Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences for the assistance of the chemical composition analysis of the gas samples.

Declaration of conflicting interests

The author(s) declared no potential conflicts of interest with respect to the research, authorship, and/or publication of this article.

Funding

The author(s) disclosed receipt of the following financial support for the research, authorship and/or publication of this article: This work was financially supported by the Chinese Academy of Sciences Key Project (Grant No. XDB10030404), the National Key Research and Development Program of China (Grant No. 2017YFA0604803), the National Natural Science Foundation of China (Grant Nos. 41572350 and 41503049), Western Light Project and the Key Laboratory Project of Gansu (Grant No. 1309RTSA041).

References

Allegre

Staudacher

Sarda

(1987) Rare gas systematics: formation of the atmosphere, evolution and structure of the Earths mantle. Earth and Planetary Science Letters 81(2–3): 127–150.

Burruss

Laughrey

(2010) Carbon and hydrogen isotopic reversals in deep basin gas: evidence for limits to the stability of hydrocarbons. Organic Geochemistry 41(12): 1285–1296.

Chen

Tang

et al. (2015) Pore and fracture characteristics of different rank coals in the eastern margin of the Ordos Basin, China. Journal of Natural Gas Science and Engineering 26: 1264–1277.

Dai

Luo

et al. (2005) Stable carbon isotope compositions and source rock geochemistry of the giant gas accumulations in the Ordos Basin, China. Organic Geochemistry 36(12): 1617–1635.

Dai

Zou

Dong

et al. (2016) Geochemical characteristics of marine and terrestrial shale gas in China. Marine and Petroleum Geology 76: 444–463.

Dang

Zhang

Tang

et al. (2016) Shale gas potential of Lower Permian marine-continental transitional black shales in the Southern North China Basin, central China: Characterization of organic geochemistry. Journal of Natural Gas Science and Engineering 28: 639–650.

Ding

Liu

(2012) Factors influencing coal bed methane reservoir in southeastern edge of Ordos Basin, China. Energy Exploration & Exploitation 30(4): 677–688.

Duan

Wang

Zheng

et al. (2008) Geochemical study of crude oils from the Xifeng oilfield of the Ordos basin, China. Journal of Asian Earth Sciences 31(4–6): 341–356.

Fan

Wang

(2017) Desorption analysis of shale and its geochemistry characteristics: A case study of the Chang 7 member shale in the central south Ordos basin. Journal of China University of Mining and Technology 46(3): 1–10.

10.

Feng

Zhang

Chen

et al. (2016) Exploitation contradictions concerning multi-energy resources among coal, gas, oil, and uranium: A case study in the Ordos Basin (western north China Craton and southern side of Yinshan mountains). Energies 9(2): 1–15.

11.

Flores

Rice

Stricker

et al. (2008) Methanogenic pathways of coal-bed gas in the Powder River Basin, United States: The geologic factor. International Journal of Coal Geology 76(1–2): 52–75.

12.

Gao

Wang

(2017) The newly discovered Yanchang gas field in the Ordos Basin, Central China. Journal of Earth Science 28(2): 347–357.

13.

Golding

Boreham

Esterle

(2013) Stable isotope geochemistry of coal bed and shale gas and related production waters: A review. International Journal of Coal Geology 120: 24–40.

14.

Guo

Liu

(1999) Transgression of Late Paleozoic Era in Ordos area. Journal of China University of Mining and Technology 28(2): 126–169.

15.

Hill

Zhang

Katz

et al. (2007) Modeling of gas generation from the Barnett shale, Fort Worth Basin, Texas. AAPG Bulletin 91(4): 501–521.

16.

Hu JY and Huang DF (1991) The Foundation of China Continental Petroleum Geology Theory. Beijing: Petroleum Industry Press, p.189.

17.

Imbus

Katz

Urwongse

(1998) Predicting CO₂ occurrence on a regional scale: Southeast Asia example. Organic Geochemistry 29(1–3): 325–345.

18.

Jarvie

Hill

Ruble

et al. (2007) Unconventional shale-gas systems: The Mississippian Barnett Shale of north-central Texas as one model for thermogenic shale-gas assessment. AAPG Bulletin 91(4): 475–499.

19.

Jiang

Feng

et al. (2016) Geologic characteristics of hydrocarbon-bearing marine, transitional and lacustrine shales in China. Journal of Asian Earth Sciences 115: 404–418.

20.

Kotarba

Rice

(2001) Composition and origin of coalbed gases in the Lower Silesian basin, southwest Poland. Applied Geochemistry 16(7–8): 895–910.

21.

Krooss

Littke

Muller

et al. (1995) Generation of nitrogen and methane from sedimentary organic matter: Implications on the dynamics of natural gas accumulations. Chemical Geology 126(3–4): 291–318.

22.

Lan

Guo

Wang

et al. (2016) Shale gas accumulation condition and favorable area optimization of the Permian Shanxi formation, Eastern Ordos Basin. Acta Geologica Sinica 90(1): 177–188.

23.

Law

Curtis

(2002) Introduction to unconventional petroleum systems. AAPG Bulletin 86(11): 1851–1852.

24.

Zhang

(2013) The origin mechanism of coalbed methane in the eastern edge of Ordos Basin. Science China – Earth Sciences 56(10): 1701–1706.

25.

Tang

Fang

et al. (2014) Distribution of stable carbon isotope in coalbed methane from the east margin of Ordos Basin. Science China – Earth Sciences 57(8): 1741–1748.

26.

Tang

et al. (2016) Continuous unconventional natural gas accumulations of Carboniferous-Permian coal-bearing strata in the Linxing area, northeastern Ordos basin, China. Journal of Natural Gas Science and Engineering 36: 314–327.

27.

Dai

Zhu

et al. (2013) Stable hydrogen and carbon isotopic ratios of coal-derived and oil-derived gases: A case study in the Tarim basin, NW China. International Journal of Coal Geology 116–117: 302–313.

28.

Pan

Xiao

Tian

et al. (2016) Geological models of gas in place of the Longmaxi shale in Southeast Chongqing, South China. Marine and Petroleum Geology 73: 433–444.

29.

Peters

(1986) Guidelines for evaluating petroleum source rock using programmed pyrolysis. AAPG Bulletin 70(3): 318–329.

30.

Qin

Song

Tang

et al. (2005) The mechanism of the flowing ground water impacting on coalbed gas content. Chinese Science Bulletin 50: 118–123.

31.

Qin

Tang

Song

et al. (2006) Distribution and fractionation mechanism of stable carbon isotope of coalbed methane. Science in China Series D – Earth Sciences 49(12): 1252–1258.

32.

Strapoc

Mastalerz

Schimmelmann

et al. (2010) Geochemical constraints on the origin and volume of gas in the New Albany Shale (Devonian-Mississippian), eastern Illinois Basin. AAPG Bulletin 94(11): 1713–1740.

33.

Sun

Tuo

Zhang

et al. (2015) Formation and development of the pore structure in Chang 7 member oil-shale from Ordos Basin during organic matter evolution induced by hydrous pyrolysis. Fuel 158: 549–557.

34.

Tang

Zhang

Ding

et al. (2016) The reservoir property of the Upper Paleozoic marine-continental transitional shale and its gas-bearing capacity in the Southeastern Ordos Basin. Earth Science Frontiers 23(2): 147–157.

35.

Wang

(1990) The cosmic chemical basis of the theory of abiogenic natural gas. Natural Gas Geoscience 1: 4–8.

36.

Wang

Chen

et al. (1994) Geochemical characteristics of gases from hot spring in seismic region. Science in China Serious B 37(2): 242–249.

37.

Wang

et al. (2015) Carbon isotopic fractionation by desorption of shale gases. Marine and Petroleum Geology 60: 79–86.

38.

Wang

Zhang

Wang

et al. (2010) Structural features and tectonic stress fields of the Mesozoic and Cenozoic in the eastern margin of the Ordos basin. Geological Bulletin of China 29(8): 1168–1176.

39.

Wang

Lei

Wang

(2015) Genesis types and sources of Mesozoic lacustrine shale gas in the Southern Ordos Basin, NW China. Energy Exploration & Exploitation 33(3): 317–338.

40.

Whiticar

(1999) Carbon and hydrogen isotope systematics of bacterial formation and oxidation of methane. Chemical Geology 161(1–3): 291–314.

41.

Wycherley

Fleet

Shaw

(1999) Some observations on the origins of large volumes of carbon dioxide accumulations in sedimentary basins. Marine and Petroleum Geology 16: 489–494.

42.

Yan

Huang

Zhang

(2015) Characteristics of marine-continental transitional organic-rich shale in the Ordos Basin and its shale gas significance. Earth Science Frontiers 22(6): 197–206.

43.

Yang

Liu

Feng

(2016) Geochemical significance of 17α(H)-diahopane and its application in oil-source correlation of Yanchang formation in Longdong area, Ordos basin, China. Marine and Petroleum Geology 71: 238–249.

44.

Yang

(2005) Tectonic and stratigraphic controls of hydrocarbon systems in the Ordos basin: A multicycle cratonic basin in central China. AAPG 89(2): 255–269.

45.

Zhang

Ellis

Ruppel

et al. (2012) Effect of organic-matter type and thermal maturity on methane adsorption in shale-gas systems. Organic Geochemistry 47: 120–131.

46.

Zhang

Shi

et al. (2015) Reservoir characteristics and controlling factors of shale gas in Jiaoshiba area, Sichuan Basin. Acta Petrolei Sinica 36(8): 926–939.

47.

Zou

Dong

Wang

et al. (2010) Geological characteristics, formation mechanism and resource potential of shale gas in China. Petroleum Exploration and Development 37(6): 641–653.

Characteristics and origin of desorption gas of the Permian Shanxi Formation shale in the Ordos Basin,China

Abstract

Keywords

Introduction

Geological setting

Sampling and experiments

Sampling

Desorption experiments

Gas geochemical analysis

Results and discussion

Geochemical characteristics

The content and constraints of desorbed gas

Origin of nonhydrocarbon gases

Origin of hydrocarbon gases

Conclusions

Footnotes

Acknowledgments

Declaration of conflicting interests

Funding

References