Geochemical characteristics of gases associated with natural gas hydrate

1 Introduction

Natural gas hydrates are crystalline compounds composed of water and gases formed under high pressure and low temperature, mainly occurring in permafrost and continental slope sediment (Kvenvolden, 1988; Dickens et al, 1995; Sloan and Sloan, 1998; Buffett and Archer, 2004). As a potential energy resource and an important part of the global carbon cycle, natural gas hydrate has been investigated intensively in recent years [e.g., (Collett et al., 2019; Ye et al., 2019; Li et al., 2021; Zhang et al., 2021b)].

As the gigantic reserve of natural gas hydrate makes it a key part of the carbon cycle with a huge potential environmental effect, understanding the origins of gases can help to constrain the global methane fluxes and potential global climate effects (Nisbet et al., 2014; Schaefer et al., 2016; Schwietzke et al., 2016). Moreover, as an unconventional energy resource, detailed composition information about gas associated with natural gas hydrate can benefit resource evaluation and optimized site selection for production test and prospective commercial exploitation (Li et al., 2018; Ye et al., 2018; Jin et al., 2020; Liang et al., 2022). Furthermore, previous studies indicate that different gas components influence the temperature-pressure phase equilibrium curve of gas hydrate and further affect the thickness of gas hydrate stability zone (GHSZ) (Tréhu AM et al., 2006; Sloan et al., 2010). Hydrates containing heavy hydrocarbon gas may be more thermodynamically stable, so that molecular composition may provide extra clues for hydrate distribution (Xiao et al., 2019).

Compare to the oil and gas which containing long-chain hydrocarbons and biomarkers , the gases associated with hydrate are with relatively simple composition (Kvenvolden, 1988; Dickens et al., 1995; Kvenvolden, 1995; Sloan and Sloan, 1998; Buffett and Archer, 2004). Therefore, the techniques can be used to infer the generation and evolution of the gases are quite limited in the earlier stage of hydrate-associated research, mainly relying on the stable isotope and molecular ratios, thus provide limited information for delineating the definite origins and sources (Bernard et al., 1977; Schoell, 1980; Whiticar, 1999; Milkov and Etiope, 2018). Fortunately, with the increase of energy demand and the need for energy transformation, more attention has been paid to the gas hydrate attribute to its clean signature with huge reserves. More hydrate samples have been obtained in recent years [e.g. (Rodrigues et al., 2019; Ye et al., 2019; Zhang et al., 2019; Lai et al., 2021a)], and several test mining of hydrate area has been implemented [e.g. (Lorenson et al., 2011; Stern et al., 2011; Kida et al., 2015; Ye et al., 2018; Liang et al., 2022)]. Furthermore, thanks to the improvement of mass spectrometry resolution and the deeper understanding of the mechanism of isotope fractionation (Eiler, 2013; Ono et al., 2014; Young et al., 2017; Dong et al, 2020), new techniques such as clumped isotope have been gradually applied to the gas geochemistry research of hydrate (Figure 1), providing valuable information for the formation temperature and kinetic secondary processes of methane (Wang et al, 2015a; Ijiri et al, 2018; Giunta et al., 2021; Zhang et al., 2021a; Lalk et al., 2022). Noble gases, which require higher quality testing methods, have also been used in recent years to study the contribution of deep mantle sources to hydrate reservoirs (Figure 1) (Ruffine et al., 2018; Moore et al., 2020; Snyder et al., 2020). Abundant samples combined with the multi-approaches make it possible to accumulate systematic and valuable data about geochemical characteristics of hydrate-associated gases for a specific area (Figure 1). However, these case studies are required further systematic discussion and summary to excavate more profound insights and provide more uniform criterions and references for future study.

FIGURE 1

Figure 1 The line of black solid dot represents the number of research articles about gas geochemistry (molecular and/or isotopic composition data) of natural gas hydrate published each year from 1970 to 2021 (data from web of science), modified from Milkov and Etiope (2018). Note that data for about 87% of all samples were published after the genetic diagrams of Bernard et al. (1977); Schoell (1983); Whiticar et al. (1986) and Milkov and Etiope (2018)were proposed. Three line of colored dot represents how those phrases (gas hydrate, clathrate and methane hydrate) have occurred in a corpus of books over the selected years (1970-2019) (data from Google N-gram viewer, (Michel et al., 2011)). We can see that use of “gas hydrate” and “methane hydrate” started to rise in 1980s, match to the publication of the genetic diagrams, while the frequency of the term "clathrate" declined steadily from the 1970s.

In this study, the geochemical data of gases associated with hydrate (including hydrate-bound gas, void gas, headspace gas and venting gas, etc.) published in recent years are compiled, and the effect of processes from the primary generation to the later accumulation of hydrate-associated gas are summarized, the methods of gas source and origin identification in recent years are discussed, to provide profound insights into the understanding of the formation mechanism and accumulation history of gas hydrate system.

2 Geochemical characteristics of natural gas hydrate

The existence of natural gas hydrate requires suitable temperature and pressure conditions, which make them mainly occurring in certain interval (GHSZ) of permafrost and marine sediment. Many factors such as gas composition, pressure gradient, geothermal gradient, and salinity affect gas hydrate stability conditions in nature. The GHSZ profiles for marine setting and permafrost environment are different (Figures 2A, B). The top and bottom of the GHSZ in these two conditions are defined by the intersection of the geothermal gradient (and/or hydrothermal gradient) with the hydrate phase boundary curve.

FIGURE 2

Figure 2 Gas hydrate stability zone (GHSZ) for gas hydrates in (A) marine environment and (B) permafrost environment, modified from (Chen and Merey, 2021).

The dataset of this study came from about 72 studies with more than 1,300 gas samples around the world (Figure 3). Of these, 133 are derived from terrestrial permafrost regions, 114 from terrestrial freshwater lakes (Lake Baikal), and the rest from marine sediments of continental margin. Most of the samples are hydrate-bound gas, void gas, headspace gas or venting gas which associated with natural gas hydrate. Almost all published isotope data of hydrate-associated gases have been compiled in Figure 4. The heaviest δ¹³C-C₁ is found at -22.5‰ in Mountain Qilian (Wang et al., 2015b) and the lightest at -102.2‰ in Amazon Fan from the distribution plot (Rodrigues et al., 2019), with an average of -61.67‰ (Figure 4A). A total of 1193 δ¹³C-C₁ data from 46 area were counted to estimate the δ¹³C-C₁ range of gases associated with natural gas hydrate. The highest frequency range of δ¹³C-C₁ appears in -70~-60‰, especially -70~ -65‰ in the frequency histogram of the δ¹³C-C₁ (Figure 4B), which may indicate that the microbial gas is quantitatively dominant in the current dataset. Samples from permafrost are with higher δ¹³C-C₁ (-55~ -30‰) compared to those from freshwater setting (-70~ 55‰), while samples from marine sediments are with widest distribution of δ¹³C-C₁ range from -102‰ to -30‰. δD-C₁ ranges from most enriched at -115‰ in the Gulf of Mexico (Sassen et al., 2001) to most depleted at -326.3‰ in Lake Baikal (Hachikubo et al., 2010), with an average value of -209.75‰ (Figure 4C). A total of 744 δD-C₁ data from same area with δ¹³C-C₁ data were counted to estimate the δD-C₁ range of gases associated with natural gas hydrate, the high-frequency range is distributed in -200 to -175‰ (Figure 4D). There is also a small high frequency band of δD-C₁ around -300‰, which represent the hydrogen isotope signature of methane generated from acetate fermentation in freshwater setting. Similar to the δ¹³C-C₁, the distribution of samples from different environment are with distinct dominated frequency interval in the frequency histogram, which manifest as samples from freshwater are with lowest δD-C₁, followed by permafrost regions, and finally marine sediment, which can be ascribed to the different sources of hydrogen in methane.

FIGURE 3

Figure 3 Location of sampled and inferred methane hydrate occurrences in marine sediment of outer continental margins and permafrost regions, modified from (Collett et al., 2009). Data of samples adopted in this study are highlighted with site name on this map.

FIGURE 4

Figure 4 (A) The distribution of δ¹³C-C₁ of hydrate-associated gas from different area around the world. (B) The frequency histogram of δ¹³C-C₁ of hydrate-associated gas counted from 1193 data. (C) The distribution of δD-C₁ of hydrate-associated gas from different area. (D) The frequency histogram of δD-C₁ of hydrate-associated gas counted from 744 data. GH, Gas Hydrate dissociated gases; Vent, Venting Gases; Void, Void gases; HG, Headspace gases; PCS, gas from Pressure coring systems (PCS).

2.1 Permafrost vs. marine sediment

Continental gas hydrate, has been identified in Messoyakha field of western Siberia, Alaska, Mackenzie delta and Qinghai-Tibet plateau [e.g., (Lorenson et al., 2011; Wang et al., 2018)], which are considered to be a major environmental concern on a number of levels since there are no methane-barrier from marine sediment and seawater compared to marine gas hydrate. As knowledge of permafrost-associated gas hydrates has grown, it has become clear that many permafrost-associated gas hydrates are inextricably linked to an associated conventional petroleum system, and that their formation history (trapping of migrated gas in situ during Pleistocene cooling) is consistent with having been sourced at least partially in nearby thermogenic gas deposits. It can also be found that methane from continental gas hydrate is more enriched in ¹³C and more depleted in D compared to that from marine settings (Figures 4A, C), which may ascribe to the mixing of microbial methane generated via acetate fermentation (Wang et al., 2018).

2.2 Microbial vs. thermogenic gas

The brief description of published geochemical characteristics of hydrate-associated gases around the world are summarized in Table S1. It can be found that hydrate with microbial origin formed by the typical acetate fermentation pathway has been identified in Lake Baikal (Figures 5A, C) (Kida et al., 2006; Hachikubo et al., 2010). The hydrates formed by the typical CO₂ reduction pathway occur in India, Blake Ridge, Black Sea, offshore northern California, Nankai Trough, offshore Oregon, Okhotsk Sea, and Ulleung Basin, etc. (Figures 5A–C) (Brooks et al., 1991; Ginsburg and Soloviev, 1997; Waseda and Uchida, 2004; Collett et al., 2008; Choi et al., 2013; Collett et al., 2019). It had been considered that most of the gases contained in natural gas hydrates mainly derived from microbial sources in the early stage of hydrate investigation, and most of the previous gas-hydrate assessments had been carried out based on that natural hydrate was formed from microbial gas. However, more and more thermogenic gas hydrates have also been recovered in later studies, for example from Caspian Sea (Lüdmann and Wong, 2003), Cascadia Margin (Pohlman et al., 2005), Gulf of Mexico (Sassena et al., 1999; Sassena et al., 2001a; Sassena et al., 2001b), Svalbard (Smith et al., 2014), west African province (De Prunel et al., 2017), NW Borneo region of the South China Sea (SCS) (Paganoni et al., 2016; Paganoni et al., 2018), Qiongdongnan of SCS (Ye et al., 2019), Shenhu of SCS (Zhang et al., 2019) and sea of Marmara (Ruffine et al., 2018), etc (Figures 5A–C).

FIGURE 5

Figure 5 Genetic diagram of δ¹³C-C₁ versus δD-C₁ (A); δ¹³C-C₁ vs. C₁/(C₂ +C₃) (B); δ¹³C-C₁ vs. δ¹³C-CO₂ (C) with dataset plotted in. Genetic diagram of δ¹³C-C₁ versus δD-C₁ (D); δ¹³C-C₁ vs. C₁/(C₂ +C₃) (E); δ¹³C-C₁ vs. δ¹³C-CO₂ (F) with secondary alteration processes (migration, mixing, biodegradation, oxidation and maturity) plotted, modified from (Milkov and Etiope, 2018). EMT-early mature thermogenic; OA-oil associated; LMT-late mature thermogenic; SM-secondary microbial; A-abiotic; F-fermentation; CR-CO₂ reduction.

It can also be seen that with the increase of samples obtained and the diversification of research methods (such as the isotopic composition of C₂₊, clumped isotopes and noble gases), the understanding of the origin of hydrate-associated gases in a certain region has gradually deepened. For example, the Shenhu area of the SCS, of which the hydrate-associated gas was originally thought to be pure microbial gas (Fu and Lu, 2010; Wu et al., 2011; Liu et al., 2015; Dai et al., 2017), has been gradually realized that it is with structurally controlled mixed gas sources with considerable thermogenic contribution in recent years, and there is a paragenetic relationship between the hydrate-associated gas and surrounding conventional oil and gas reservoirs (Zhang et al., 2019; Lai et al., 2022; Liang et al., 2022). New subtype of gases, such as secondary microbial gases generated by hydrocarbon biodegradation, has been widely recognized in more areas with the deepening of the understanding of the gas generation (Figures 5A–C) [e.g., (Milkov, 2018; Ruffine et al., 2018; Lai et al., 2022; Li et al., 2022)].

3 Primary origins of hydrate-associated gases

Gases bound in hydrate usually formed by biodegradation of organic matter, which includes bacterial gas (or called microbial gas) produced by bacterial processes and thermogenic gas formed through thermochemical reactions (Schoell, 1983). The characteristics of biogenic gas are controlled by the type and thermal maturity of organic matter, i.e. kerogen type, burial history and geothermal gradient (Tissot et al., 1974; Tissot and Welte, 1984; Whiticar, 1994).

The origin material of natural gas is divided into sapropelic type, which are mainly type I/II kerogen and dominated by marine source organic matter, and humic type which are mainly type III kerogen and dominated by terrestrial organic matter (Van Krevelen, 1961). The natural gas generated by sapropelic organic matter is named oil-type gas, and that by humic organic matter is named as coal-type gas. Study of organic matter in hydrate-bearing sediment of Okinawa trough suggested that terrestrial organic matter is more prone to the formation of microbial gases as compared with marine organic matter (Saito and Suzuki, 2007). However, Dai et al. (2017) proposed that most of the gas-forming hydrates are oil-type gas from marine organic matter, and coal-type gas has only been reported in Qilian Mountain and offshore Vancouver island (Wang, 2010; Cao et al., 2012).

The thermal maturation stages of organic matter are labelled (1) Immature (diagenesis), the initial thermal mature stage where microbial gas is dominated; (2) Mature (catagenesis), the intermediate stage where oil and methane are generated from kerogen decomposition; (3) Post-mature (metagenesis), the final stage where almost pure methane (dry gas) formed mainly from thermal cracking of oil and bitumen (Tissot and Welte, 1984; Wiese and Kvenvolden, 1993). Therefore, the natural gas component changes from microbial dry gas to thermogenic wet gas and then to thermogenic dry gas in the immature, mature and over-mature stage of organic matter evolution (Tissot and Welte, 1984; Wiese and Kvenvolden, 1993).

4 Secondary processes after gas generation

After being generated in source rocks, natural gases may experience a series of secondary processes, such as mixing, migration, oxidation and biodegradation, etc., before the formation of reservoir. The primary geochemical characteristics of the gases can be obscured by these secondary processes, resulting in isotopic and molecular compositional fractionation. As a result, it is necessary to identify these secondary processes and their effects, to properly interpret the origins and sources of the gases.

4.1 Migration

Microbial methane produced in the GHSZ alone is not sufficient for the accumulation of concentrated gas hydrate in most cases. Most of the allochthonous gas in the GHSZ might have been migrated from the deeper sediments, mainly involving three kinds of processes: (1) diffusion; (2) migration of water-dissolved gas; (3) buoyancy of free gas. Diffusion is quite slow, unlikely to bring up sufficient gas to form highly saturated hydrate reservoirs in most cases (Xu and Ruppel, 1999). However, the latter two are relatively efficient processes.

Diffusion-associated fractionations of isotope and molecular composition of hydrocarbons are expected to occur as a function of mass and are thought to behave “chromatographically”, by which lighter isotopes and hydrocarbons move more quickly than their heavier counterparts (Thompson, 1979; Leythaeuser et al., 1982; Choi et al., 2013). It is also found that ¹²C-¹²C bond is more prone to breakage than ¹²C-¹³C bond and the compounds with heavy carbon isotope ¹³C is more easily absorbed by rocks, minerals and organic matters (Chanton, 2005). As a result, ¹³C_-CH4 and D_-CH4 for a diffused gas are depleted relative to its source, while C₁/(C₂+C₃) is relatively increased (Coleman et al., 1977; Prinzhofer and Pernaton, 1997; Zhang and Krooss, 2001; Schloemer and Krooss, 2004). Coleman et al. (1977) validated the effect of diffusion on the molecular composition of gases and proposed that C₂₊ hydrocarbons can be entirely stripped off from the migrated gases. It is proposed that the migration via diffusion can cause measurable carbon isotope fractionation of more than 5‰ (Chen, 1994; Prinzhofer and Pernaton, 1997). Both simulation and experimental results reveal that the fractionation by diffusion is affected by TOC content and porosity and permeability of rock, the migration pathway and the type of migrating gas, etc. (Galimov, 1967; Craig, 1968; Gunter and Gleason, 1971; Stahl, 1977; Chen, 1994; Zhang and Krooss, 2001; Li et al., 2003).

There are still debates on whether isotopic fractionation occurs or not in the process of natural gas migration other than diffusion, although most studies suggest that there is no isotope fractionation during migration (Stahl and Carey, 1975; Coleman et al., 1977; Fuex, 1980; Faber and Stahl, 1984; Zhang and Krooss, 2001). The isotopic compositions of natural gases, recovered from different depths of the same well shows no obvious difference (Stahl and Carey, 1975; Coleman et al., 1977; Faber and Stahl, 1984). Schoell proposed that the migration of natural gas would not cause the change in δ¹³C_-CH4, insteadly the isotopic compositions of natural gases are controlled by the type and thermal evolution of original organic matter (Schoell, 1983; Schoell, 1984). Experiment and numerical simulation conducted by Fuex (1980) showed that migration fractionation of methane was almost negligible, and the most likely cause of this insignificant fractionation was the difference in water solubility between ¹²CH₄ and ¹³CH₄, and in most cases such fractionation would not exceed 1-permil. It is also suggested that depletion in methane carbon isotope is caused by bacterial activities rather than by migration (Fuex, 1980; Faber and Stahl, 1984). Based on the discussions above, migration is expected to cause thermogenic gas zone to shift upward in the C₁/(C₂+C₃) versus δ¹³C_-CH4 diagram, corresponding to an increase in C₁/(C₂+C₃) ratio but no significant change in δ¹³C_-CH4 (Figure 5E) (Bernard et al., 1977).

4.2 Mixing

Mixing of natural gases, which can be from the identical source rock at varying maturity stages or different source rocks, and biogenic and abiogenic origins, is a common phenomenon (Whiticar, 1994). The mixing of microbial and thermogenic gas has been well recognized in gas hydrates in Shenhu area of South China Sea (SCS) (Zhang et al., 2019), Norwegian Sea (Vaular et al., 2010) and Japan Sea (Waseda and Iwano, 2008). In recent years, the mixing of thermogenic gas with secondary biodegraded gas has also been identified in areas such as Western High of Sea of Marmara (Ruffine et al., 2018).

The molecular and isotopic composition of natural gas are adopted to identify mixing and to determine the composition and contribution of each gas-endmember (Schoell, 1983; Chung et al., 1988; Whiticar, 1994; Prinzhofer and Huc, 1995). As shown in Figure 3A, mixing of microbial and thermogenic gas can be identified by the carbon isotope of methane (δ¹³C-C₁) and the dry coefficient of the gas (C₁/(C₂+C₃)) (Figure 5E) (Bernard et al., 1977), and a linear relationship between the two endmembers has been recognized, changing strictly with the mixing ratio in the δ¹³C-C₁ versus δD-C₁ diagram (Figure 5D). Prinzhofer and Pernaton (1997) proposed that the mixing of two gas endmembers result in a straight line in the plot of C₂/C₁ versus δ¹³C and an exponential line in the plot of log (C₂/C₁) versus δ¹³C. Prinzhofer et al. (2000) indicated that in any plot where the ratio of two numerators with a common denominator (for example, δ¹³C-C₁, δ¹³C-C₂ and δ¹³C-C₃) is drawn, the mixing between the two end-members is on a straight line, and the linear relationship becomes more pronounced when isotope of C₂₊ gases is applied. Chung et al. (1988) proposed “natural gas plot” based on the semi-linear relationships of the carbon isotopic compositions of n-alkanes in pure thermogenic gases, which can help to estimate the relative contribution of microbial gas or thermogenic gas in a two end-member mixing model, after the δ¹³C of thermogenic methane is obtained by extrapolating the line of isotopic values of C₂₊ gases. This method has been widely used in hydrate gas studies [e.g., (Hachikubo et al., 2015; Lai et al., 2021a)].

4.3 Hydrate formation and dissociation

The gas hydrate system has always been in a dynamic equilibrium state and is extremely sensitive to environmental conditions, especially temperature and pressure conditions change, driving forces leading to its dissociation have been primarily ascribed to event such as pressure reduction (e.g., (Teichert et al., 2003, Watanabe et al., 2008), temperature rise [e.g. (Cremiere et al., 2016, Kennett et al., 2000, Phrampus and Hornbach, 2012)], salinity changes (Riboulot et al., 2018) and glacial-interglacial transition (Chen et al., 2019, Deng et al., 2021). Isotopic and molecular fractionation may occur during the hydrate formation, dissolution and dissociation, so it is necessary to clarify whether the isotope fractionation is caused by hydrate crystallization itself. Laboratory studies by Hachikubo et al (2008) found that the δD of hydrate-bound gases is several permil depleted than that of residual gas, while there was no significant difference in δ¹³C. Nevertheless, the difference in δD is not so significant that affects the determination of gas origin. The effect of temperature on isotopic fractionation was also studied, and it was found that the fractionation was more evident with temperature decreasing (Hachikubo et al (2008), which was confirmed by Kimura et al. (2021). Experimental study from Luzi et al (2011a) has shown that hydrate formation has no significant effect on the carbon isotope ratios for CH₄ hydrate, whereas a noticeable δ¹³C depletion was observed with CO₂ hydrates compared to the gas phase. Similar isotope depletion in hydrate phase was observed by Kimura et al. (2021). However, contrary experimental results from Chen et al. (2018) indicates that heavy isotopes tend to preferentially enter the hydrate phase during the formation of CO₂ hydrate and the carbon isotope fractionation is less intensive than that of oxygen and hydrogen. A comparison of stable isotope ratios of hydrate-bound and sediment gases, which were collected at the same depth of the same core from Lake Baikal, was performed, revealing that the δ¹³C_-CH4 and δD_-CH4 of the hydrate-bound gas were 1-2‰ and 5‰ smaller than the sediment gas, respectively (Kimura et al., 2020). The hydrogen isotope fractionation was in good agreement with the prediction from the experimental results of synthetic methane hydrate (Hachikubo et al., 2008), while the reason for the isotopic fractionation in ¹³C was still unknown. Lin and Zeng (2010) discovered that the molecular compositions are differentiated during hydrate formation, methane content decreases in hydrate phase as compared with wet gases (C₂₊) due to the difference in combination ability with water.

Lapham et al. (2012) experimentally studied the possible fractionation during hydrate dissolution or decomposition (two different physical processes), and it was confirmed that there is no isotope fractionation during both processes. Lai et al. (2021b) conducted a step-wise depressurization experiment with hydrate-bearing sediment to study the possible changes in the molecular and isotopic composition of gases released in depressurization process, indicating that no significant change in carbon isotopic composition while heavy hydrocarbons released mainly in the later stage of hydrate dissociation.

4.4 Biodegradation

When migrating upward into the shallow sediments, thermogenic gases containing certain amount of C₂₊ components might experience biodegradation with the involvement of microorganisms, and their original characteristics would be changed while yielding secondary methane (Head et al., 2003; Jones et al., 2008; Knittel and Boetius, 2009; Jones et al., 2010; Gao et al., 2013; Mesle et al., 2013; Schlegel et al., 2013). As microorganisms preferentially consume C₂₊ gases and produce secondary microbial C₁ as the terminal product, C₁ will be gradually accumulated and the ratio of C₁/(C₂+C₃) will be increased (Figure 5D) (Zeikus, 1977; Larter et al., 2005; Boreham and Edwards, 2008). Generally, methane generated from hydrocarbon biodegradation is relatively enriched in ¹³C compared to methane from primary methanogenesis (Valentine et al., 2004; Milkov and Dzou, 2007). It is also found that, biodegradation preferentially consumes ¹²C of propane and results in the enrichment of ¹³C in residual propane while the isotopic composition of ethane is not changed (James and Burns, 1984). As a result, the carbon isotopic compositions of hydrocarbon components in original thermogenic gases generally display a smooth progressive distribution pattern from C₁ to C₅, while those of biodegraded gases exhibit a serrated configuration, especially with unique ¹³C enrichment of propane (James and Burns, 1984). Moreover, as CO₂ with ¹²C derived from biodegraded hydrocarbons is preferentially converted into secondary microbial methane, the residual CO₂ becomes more enriched in ¹³C (> +2‰) (Figures 5C, F) (Lillis and Magoon, 2007). Such significant enrichment in ¹³C of CO₂ is unique, and it can be a proxy of biodegradation degree. Typical gas hydrates, which contain biodegraded-gases with enriched ¹³C isotope composition of CO₂ (+25‰), have been reported in the Western high of Sea of Marmara (Ruffine et al., 2018).

4.5 Oxidation

Hydrate-associated gases will be oxidized by anaerobic or aerobic process while upward escaping, and the dominant process depends on the surrounding redox conditions. For aerobic oxidation, both enriched cultures with methane-oxidizing bacteria and analytical results of natural gas samples have suggested that oxidation can lead to the decrease in C₁ content and enrichment in ¹³C and D of residual C₁ (Figures 5D–F), because the C₁ with lighter isotope is preferentially oxidized during this process (Coleman et al., 1981; Etiope et al., 2011; Daskalopoulou et al., 2018). Coleman et al. (1981) proposed that the extent of isotope fractionation is associated with temperature, and the change in δD value of methane is 8~14 times greater than that of δ¹³C value. Kinnaman et al. (2007) suggested that the isotope fractionation becomes less intensive with the increment of carbon number (i.e., C₁>C₂>C₃>C₄), and the degree of isotope fractionation appears insignificant with substrate decreasing.

For anoxic sediments, the anaerobic oxidation of methane (AOM) predominates with the involvement of microorganism (Barnes and Goldberg, 1976; Reeburgh, 1976). Variation in methane isotopic composition has been observed in active AOM marine sediments, and it has been attributed to the difference in sulfate availability (Borowski et al., 1997; Pohlman et al., 2008; Yoshinaga et al., 2014). Batch enrichment cultures revealed that at seawater sulfate concentrations (28 mM), AOM will induce kinetic isotope fractionations, resulting in the enrichment of ¹³C and D in the residual methane (Holler et al., 2009; Ono et al., 2021). In contrast, at low sulfate concentrations AOM results in ¹³C-depletion in the remained methane and were explained as isotopic equilibration between methane and inorganic carbon mediated by AOM (Yoshinaga et al., 2014).

5 Discussion

Accurate depict of the formation and accumulation process of the hydrate-associated gas requires information obtained from various aspects. Development of both conventional and novel techniques make it possible to deepen our understanding of the gas geochemistry study. Here, we discuss the hydrate-associated gas geochemistry from three aspects via a complete overview of the state of the art, recent research breakthroughs, and areas of continued controversy.

5.1 Stable isotope & Gas composition

5.1.1 Developments

Stable isotope and molecular composition have always been basic properties of the gases that reflect their origins and sources. The most commonly used method to interpret the origin of gases is the plot of C₁/(C₂+C₃) versus δ¹³C_-CH4, known as “Bernard plot” because it was originally proposed by Bernard et al. (1976). Based on the analytical results of natural gases, Bernard et al. (1976) noticed that the microbial gas always is with a higher dry coefficient (C₁/(C₂+C₃) > 1000) and lighter δ¹³C_-CH4 (δ¹³C_-CH4<-60‰), while thermogenic gas usually is with lower dry coefficient (0< C₁/(C₂+C₃)< 50) and heavier δ¹³C_-CH4 (δ¹³C_-CH4 >-50‰). Schoell first proposed of using the carbon and hydrogen isotopes of methane to recognize the origin of hydrocarbon gases (Schoell, 1980; Schoell, 1983). The genetic diagram includes microbial gases from marine (δ¹³C< -60‰, δD -200‰ ~ -150‰) and terrestrial environment (δ¹³C< -60‰, δD -250‰ ~ -200‰), oil-associated thermogenic gases (δ¹³C -60‰~ -25‰, δD -300‰~ -150‰) and non-oil-associated gases (δD >-150‰). Whiticar further modified the diagram by merging all thermogenic gases into one area, and specified microbial gases into CO₂ reduction and acetate fermentation (Whiticar et al., 1986; Whiticar, 1999). Gutsalo and Plotnikov (1981) proposed the first genetic diagram based on the carbon isotopic compositions of methane and carbon dioxide (δ¹³C_-CO2 vs. δ¹³C_-CH4), which grouped the gases into abiogenic gas, microbial gas and thermogenic gas. Milkov, 2011 added to the diagram the genetic region of secondary microbial gases from oil biodegradation, and Etiope et al added new region of abiogenic CH₄ to this genetic diagram (Etiope and Lollar, 2013; Etiope and Schoell, 2014; Etiope, 2017).

Milkov and Etiope (2018) revised the three plots based on the data from more than 20,000 natural gas samples published in recent decades, updating a more detailed classification of gas origins (Figure 5). In addition to the above classification diagram, other information from geological geochemical or even experimental studies can benefit to figure out the gas origin. The primary microbial gases are characterized by the composition with C₁-C₃ hydrocarbons only, which is supported by the results from laboratory experiments that microbes can merely generate these three hydrocarbons (Oremland et al., 1988; Hinrichs et al., 2006). The geological setting can provide boundary condition to identify the microbial gas, such as the absence of oil in the sediment or reservoir. Similarly, thermogenic gases are usually associated with conventional oil reservoir and characterized by the presence of all the methane homologues (i.e., C₁-C₅).

5.1.2 Recent advances

Most studies of hydrate-related gases stop at distinguishing whether the gas is thermogenic derived from deep sources or microbial from shallow methanogenesis. For gases from deep sources, there are few ways to identify the specific source rocks, which constrain the understanding of the generation and accumulation processes of gas hydrate deposits for a specific area.

Rooney et al. (1995) proposed that the relationship between methane and ethane in the early stages of thermogenic gas generation can be described with the following equation Eq (1):

$\begin{array}{ll}\delta C_2 = -0.5 \left(\delta C_{org} – \delta C_1\right)+ \delta C_{org}& (1)\end{array}$

where δC_org is referred to δ¹³C of the organic matter; generally -27‰ taken for terrestrial sources, and -20‰ for marine sources (Rooney et al., 1995; Lorenson and Collett, 2018). Lorenson and Collett (2018) studied δC₁ and δC₂ of hydrate gas offshore India and found that gas from KG basin is mainly microbial, while those from the deep Mahanadi Basin are mainly derived from the gas-prone terrestrial organic matter (Figure 6A). Liang et al. (2022) proposed that microbial and thermogenic gases associated with gas hydrate from the Shenhu area were derived from marine and terrigenous organic matter, respectively, based on the isotopic composition of C₁ and C₂ (Figure 6A). The integrated isotopic values of C₁, C₂ and C₃ can better identify the gas origins and the types of their precursor organic matter (Figure 6B). Liang et al. (2022) pointed out that most of the hydrate containing gases in Shenhu area fell into the sapropelic gas area (Figure 6B), which is close to conventional gas reservoirs in the plot (area IV in Figure 4), indicating for the first time that the thermogenic gas in hydrate is cogenetic with conventional oil and gas reservoirs in Panyu low uplift of Baiyun Sag. Above studies emphasize the importance of high-precision isotope measurement of C₂₊ components in hydrate-associated gases, which can provide clues for the identification of the source rocks of the gases.

FIGURE 6

Figure 6 (A) Relationship of different types of organic matter in the source rocks and hydrate-associated gas. The diagonal lines are adapted from  (Lorenson and Collett, 2018). VG-Void Gas, PCS-pressure core gas; GH-Gas Hydrate dissociated gases; NG-Natural gas. (B) Plot of the δ¹³C₁, δ¹³C₂, and δ¹³C₃ values of the hydrate-bound gas samples. The genetic diagram is adapted from (Dai, 1992).(I-Humic type gas; II-Sapropel type gas; III-Gas mixture with the reversal of carbon isotope; IV-Humic type gas and sapropel type gas; V-Biogenic gas). .

In addition, detailed organic geochemistry, microbial and geological investigation have been proved to be robust tools to provide extra clues for gas origins and sources in recent years (Lai et al., 2022; Li et al., 2022; Lin et al., 2022). Presence of biomarkers of deeply buried thermogenic hydrocarbons and microbial communities associated with hydrocarbon degradation are remarkable signatures to identify the secondary biodegraded gas. This kind of integrated study should be widely used in the future research of hydrate-associated gases (Lai et al., 2022).

5.1.3 Unresolved questions

Although several methods have been proposed for the identification of the origins of hydrate-associated gas, sometimes it is still difficult for a specific case because there are unclear boundaries and overlaps between different classifications (Figure 5) (Martini et al., 1996; Prinzhofer and Pernaton, 1997; Martini et al., 1998; Valentine et al., 2004; Etiope and Schoell, 2014; Smith et al., 2014). The molecular and isotopic fractionation caused by post-generation processes makes the identification of gas origins more challenging (Prinzhofer and Pernaton, 1997; Martini et al., 1998; Whiticar, 1999). In addition, empirical diagrams are often proposed through a large amount of statistical data, which may not applicable to hydrate samples from all geological settings. Empirical formulas often ignore the effects from secondary process like mixing, migration and biodegradation. However, these processes often obscure the original signal of the gases, so it is better to interpret the data with other aspects of evidence, such as organic geochemistry of hydrate-bearing sediment, geophysics data, etc.

It is also an unsolved problem to quantitatively identify the contributions of different gas sources. Especially for the mixed-origins gas hydrate, the contribution proportion of shallow in-situ microbial gas and allochthonous thermogenic gas is still a difficult problem. Sun et al. (2020) reconstructed a geological model combining seismic, well and geological interpretation to predict hydrocarbon generation, migration and formation of gas hydrate in Shenhu area. The modeling shows that about 80% of the methane-forming hydrate is with thermogenic source and the total organic carbon (TOC) content is considered to be important factor related to biogenically-sourced gas hydrate distribution. However, TOC and hydrocarbon-generation index (HI) are important parameters that considered in this study, more relevant parameters about source rocks especially biogenic source rocks should be evaluated in the future studies.

5.2 Clumped isotope

5.2.1 Developments

Additional proxies are required to help distinguish between different sources and post-generation processes. As a novel technique established in the past 10 years, methane clumped isotopes are with potential to improve our understanding of gas origins. Clumped isotopes are referred to multiply substituted isotopologues with two or more rare isotopes e.g. ¹³CH₃D and ¹²CH₂D₂ for methane (Eiler, 2007; Eiler, 2013). The first study of methane clumped isotopes was conducted at Caltech on ultra-high resolution isotope mass spectrometry (Thermo fisher, Ultra), but upon that time only a total Δ18 signal could be available, unable to distinguish ¹³CH₃D from ¹²CH₂D₂ (Stolper et al., 2014b). Later, measurement of ¹³CH₃D was also achieved using Tunable Infrared Laser Direct Absorption Spectroscopy (TILDAS) at MIT (Ono et al., 2014). The recognition of both ¹²CH₃D and ¹³CH₃D signals on a single measurement was succeeded for the first time with a higher resolution mass spectrometry (Nu, Panorama) in 2016 at UCLA (Young et al., 2016; Young et al., 2017), although Ultra and TILDAS also achieved this function in the following years (Eldridge et al., 2019; Gonzalez et al., 2019; Dong et al., 2020; Dong et al., 2021). Recently, a commercial instrument (Ultra), which is developed by Thermo-Fisher , has been successful in clumped isotope measurement in Tokyo Institute of Technology, indicative of the maturity of this technology (Zhang et al., 2021a). Methane clumped isotope analysis quantify the abundances of isotopologues of methane relative to the ideal gas state of random distributions of isotopes over methane molecules (Young et al., 2016; Douglas et al., 2017; Young et al., 2017). Clumped isotopes of methane may primarily record its formation or equilibration temperature if the isotopologues are thought thermally equilibrated when both the Δ¹³CH₃D and Δ¹²CH₂D₂ values are on the thermodynamic equilibrium curve in Figure 7 (Stolper et al., 2014a; Webb and Miller, 2014; Wang et al., 2015a). This method is established based on the theory of isotopologue exchange reaction [Eq (2)], of which the equilibrium is controlled by temperature.

$\begin{array}{ll}{ }^{13}C{H}_4 +{ }^{12}C{H}_{3}D \to { }^{13}C{H}_{3}D+ { }^{12}C{H}_4& (2)\end{array}$

FIGURE 7

Figure 7 (A) Compile of the published clumped isotope of hydrate associated gases plotted in thermodynamic equilibrium curve in Δ¹²CH₂D₂ vs. Δ¹³CH₃D space (both axes are in per mil). Mixing and diffusion trend are adopted from (Douglas et al., 2016), oxidation trend from (Douglas et al., 2017). (B) Cross-plot of the published clumped isotope (Δ¹³CH₃D) and conventional stable isotope (δ¹³C-C₁) of hydrate associated gases (both axes are in per mil), modified from (Lalk et al., 2022). SG-Sedimentary Gases.

The formation temperature of methane obtained by this method provides crucial clues for its origin. Microbial gas is formed at low temperature (usually<75°C) via biogeochemical processes in subsurface sediments, while thermogenic gases generated from pyrolysis of organic matter usually occur at high temperatures (usually>150°C). Abiotic gases involve a variety of reactions, which can be classified as reaction in mantle, magmatic system (~>600°C) or water-rock interaction (~50-500°C).

5.2.2 Recent advances

Clumped isotopologue analyses have been applied to studying hydrate-associated methane from Hydrate Ridge on Cascadia Margin (Wang et al., 2015a), Kumano Basin mud volcano in Nankai accretionary complex (Ijiri et al., 2018), Japan Sea (Zhang et al., 2021a), Sea of Marmara (Giunta et al., 2021), as well as 46 samples from the other 11 regions in the world (Lalk et al., 2022) (Figure 7A, B).

The Δ¹³CH₃D of microbial methane from both porewaters and gas hydrates recovered from sediments in the northern Cascadia margin yielded methane formation temperature ranging from 12°C to 42°C (Figure 7B) (Wang et al., 2015a), which is in accordance with the surrounding environment. Similarly, clumped methane isotopologues of the gases from Kumano forearc basin in Nankai accretionary complex indicate that ~90% of methane is produced microbially at an estimated temperature between 16° and 30°C (Figure 7B), consistent with a relatively shallow microbial source in the sediments of 300-900mbsf (Ijiri et al., 2018). However, from clumped isotopes the formation temperatures of methane are calculated to be 15 to 170°C for the methane gases from the Sea of Japan (Figures 7A, B). By combining clumped isotope results with other traditional approaches, the microbial methane is quantified to be 20-80% compared to the thermogenic (Zhang et al., 2021a). Giunta et al. (2021) measured ¹³CH₃D and ¹²CH₂D₂ of methane from cold seeps emanating at the seafloor of Sea of Marmara (SoM) (Figures 7A, B), and it is found that the isotopic characteristics of methane in SoM cannot be simply explained by mixing of multiple reservoirs but appears to be affected to varying degrees by bond re-equilibration with clay minerals (Ruffine et al., 2018). This might imply that the temperature obtained from clumped isotope represents the re-equilibration condition of post-generation rather than the actual formation temperature of methane. Lalk et al. (2022) analyzed 46 gas hydrates and associated gases from seepages of different types (cold seeps, oil seeps, pockmarks, and mud volcanoes) in 11 regions around the world (Figure 7B), discovering that the formation temperatures of methane associated with cold seeps and pockmarks locate in the microbial range between 15°C and 70°C. However, the temperature of methane gases from oil-associated gas hydrates are estimated to be 50°C to 120°C, corresponding to secondary methane generated by oil biodegradation. The methane gases associated with mud volcanoes are with a wide range of Δ¹³CH₃D values, and the correspondent temperatures of methane formation are not consistent with the conditions indicated by conventional proxies, suggesting their diverse origins which could be attributed to the tectonic settings (Lalk et al., 2022).

5.2.3 Unresolved questions

Clumped isotopes with equilibrium signals can provide important information for temperature and can be used as thermometers (Stolper et al., 2014a). However, not all data measured in reality are ideally in equilibrium. Most of the temperature results calculated with clumped isotopes of thermogenic gases are consistent with those of their surrounding environment (Douglas et al., 2017; Young et al., 2017; Stolper et al., 2018; Giunta et al., 2019; Giunta et al., 2021), indicating that clumped isotope can reflect the formation temperature of methane. However, in laboratory based thermal experiments, such as pyrolysis of shale, coal, or hydrocarbons, significant non-equilibriums in clumped isotopes have been observed (Shuai et al., 2018; Dong et al., 2021), which is considered to be a statistical combinational effect or kinetic isotope effects (KIE) during pyrolysis. Simulating experiments also reveal that hydrocarbons may approach equilibrium in clumped isotope with maturity increasing (Xia and Gao, 2019; Dong et al., 2021).

Compared to thermogenic gas, the values of clumped isotopes of microbial methane are in a wide range. The temperature, deduced from clumped isotopic composition of microbial methane generated in laboratory culture experiments, is much lower than its actual culture condition (Stolper et al., 2015; Wang et al., 2015a; Young et al., 2017; Gruen et al., 2018; Giunta et al., 2019; Douglas et al., 2020). The extremely depletion in ¹²CH₂D₂ is mainly ascribed to quantum tunneling effect or combinatorial effects of 4 hydrogen atoms of methane from different reservoirs or experiencing different fractionations (Young et al., 2017; Cao et al., 2019; Young, 2019; Taenzer et al., 2020), while the moderate ¹³CH₃D depletion is mainly attributed to quantum tunneling or kinetic isotope effect of methanogenesis (Wang et al., 2015a; Cao et al., 2019; Young, 2019; Douglas et al., 2020). In surface environments such as cattle rumen and freshwater ecosystems, disequilibrium clumped isotope characteristics of biogenic methane were widely reported, exhibiting obvious kinetic signals, and corresponding temperatures were much higher than the actual ambient condition (Stolper et al., 2015; Wang et al., 2015a; Douglas et al., 2016; Young et al., 2017; Ash et al., 2019; Giunta et al., 2019; Douglas et al., 2020). However, methane gases taken from marine sediments usually show a relatively consistent temperature compared to the ambient condition (Figures 7A, B) (Inagaki et al., 2015; Wang et al., 2015a; Young et al., 2017; Ijiri et al., 2018). The mechanisms for the equilibration of methane clumped isotopes in marine sediments can involve the processes of methanogenesis or oxidation of methane. For methanogenesis, the rates of methane formation and enzyme reversibility are recognized as the two main factors affecting the kinetics of clumped isotope equilibration based on the culturing experiments and observations on natural samples (Stolper et al., 2015; Wang et al., 2015a; Douglas et al., 2016; Douglas et al., 2020). For oxidation of methane, reversible bond reordering in the AOM process was identified as the key process controlling the equilibration of clumped isotopes (Ash et al., 2019; Ono et al., 2021).

In addition to the above disequilibrium condition, secondary post-generation processes such as oxidation, migration and mixing of methane can also alter the original clumped isotope signal (Stolper et al., 2015; Wang et al., 2015a; Yeung et al., 2015; Young et al., 2017; Giunta et al., 2019; Labidi et al., 2020; Giunta et al., 2021; Warr et al., 2021). Mixing may lead to a non-linearity trajectory in the Δ¹³CH₃D-Δ¹²CH₂D₂ diagram (Figure 7A) (Douglas et al., 2016; Young et al., 2016), with a curvature depending on bulk isotopic compositions (δ¹³C and δD) of end-members. The curvature of the mixing line is negligible when the values of end-member δD and δ¹³C are close, but it becomes progressively significant when the values of end-member δD and δ¹³C become more different (Stolper et al., 2015; Douglas et al., 2016). Diffusion of methane, either in the condition of vacuum or interaction with particles, is predicted to favor the light isotopologues to be enriched in diffused gas as compared with the residual gas (Figure 7A). Two variants of Δ¹³CH₃D and Δ¹²CH₂D₂ should be with an integer mass ratio of 18/16, so any fractionation caused by molecular mass, like diffusion, should display a 1:1 slope in this space (Douglas et al., 2017). Douglas et al. (2017) proposed that atmospheric chemical reactions of methane with OH.^-, Cl.^- would increase the abundance of ¹²CH₂D₂ and ¹³CH₃D (Figure 7A), but their enrichment degrees are different. Microbial methanotrophy, including aerobic and anaerobic oxidation of methane, can change initial clumped isotope signatures of methane as well (Wang et al. 2015a; Ash et al., 2019; Young, 2019; Ono et al., 2021). For aerobic oxidation of methane, Wang et al. (2016) found a decrease in Δ¹³CH₃D and a significant increase in δD and δ¹³C values of CH₄ in bio-simulation experiments under aerobic condition. While for anaerobic oxidation of methane (AOM), reversible bond re-ordering is proposed to be the key process leading to near-equilibrium values based on observations in natural samples (Ash et al., 2019). Laboratory culture experiments (Young, 2019; Ono et al., 2021) qualitatively confirm the role of AOM in modifying methane clumped isotope signatures, but some of these experimental results do not quantitatively agree with the observations in natural samples. Ono et al. (2021) reported that Δ¹³CH₃D values of residual CH₄ were 3.1‰ higher than the expected equilibrium values, which might be associated with KIE resulted from rapid AOM rates during incubation, while Young (2019) observed distinct bond re-ordering trends in Δ¹³CH₃D vs. Δ¹²CHD₂ plot under changing sulfate concentrations. The specific mechanism of how AOM catalyzes bond re-ordering requires further investigation.

5.3 Noble gases

5.3.1 Developments

Noble gases are chemically inert, so their elemental ratios can be changed only by physical processes but not by microbial activities and chemical reactions. Based on these specific properties, methods are established to decipher complex geochemical processes (Winckler et al., 2000). Noble gases are well constrained in different units of the earth surface system, coming from three-endmember sources: (i) atmosphere, or air-saturated water (ASW): e.g., ²⁰Ne, ³⁶Ar, ³⁸Ar, ⁸⁴Kr, ¹³²Xe; (ii) ³He-rich mantle; and (iii) crustal, rich in radiogenic noble gases accumulated by radioactive decay, e.g. U + Th → ⁴He^*, ²¹Ne^*, ¹³⁶Xe^* ; ⁴⁰K → ⁴⁰Ar^* (Ballentine and Burnard, 2002).

The elemental and isotopic compositions of noble gases facilitate additional constraints on the genetic origins of and semiquantitative estimation of the biogenic and thermogenic contributions of natural gas. Noble gases are also employed to study the dynamics of fluid migration, estimate the residence time of hydrocarbon gases in reservoir, and specify post-genetic processes that might have modified hydrocarbon composition (Zhou et al., 2005; Zhou and Ballentine, 2006; Schlegel et al., 2011; Hunt et al., 2012; Darrah et al., 2014; Darrah et al., 2015; Wen et al., 2015; Barry et al., 2016; Harkness et al., 2017).

Previous experimental and theoretical studies have demonstrated that formation of hydrate will result in fractionation to certain degree between noble gases, as reflected by the enrichment of heavier noble gases in gas hydrate (Nikitin, 1937; Barrer and Stuart, 1957; Hunt et al., 2013). Noble gases studies of gas hydrates from Blake Ridge show that the formation of hydrate is characterized by the Xe enrichment in hydrate phase due to noble gas fractionation (Dickens and Kennedy, 2000). Natural gas hydrates from Hydrate Ridge are almost with no He and Ne, but contain high Ar and Kr and Xe, suggesting that the heavier noble gases were preferentially entered gas hydrate structure compared with the lighter noble gases, which could be ascribed to the thermodynamic effect or solubility difference (Winckler et al., 2002). The experimental results of synthesizing hydrate of mixed methane and noble gases (He, Ne, Ar, Kr and Xe) reveal that Kr and Xe are enriched relative to Ar but without detectable He and Ne in hydrate, also indicative of the effect of mass fractionation of noble gases in hydrate formation process (Hunt et al., 2011; Hunt et al., 2013).

5.3.2 Recent advances

As discussed in previous sections, traditional methods are with limitations to delineate gas origins, noble gases can provide additional clues about the thermal maturity of natural gases and the migration of allothogenic fluids. Crustal noble gases like ⁴He, ²¹Ne and ⁴⁰Ar are present in high concentrations in thermogenic gases, whereas recently formed microbial gases are nearly devoid of radiogenic noble gases (Hunt et al., 2012; Darrah et al., 2015; Wen et al., 2015; Harkness et al., 2017). On the contrary, the increase of atmospherically derived gases like ²⁰Ne and ³⁶Ar seems to correspond to an elevated proportion of microbial gas (Ballentine et al., 2002; Ballentine and Burnard, 2002). Furthermore, the ³He/⁴He (shown as R/Ra, where R is the ³He/⁴He in a gas sample and Ra is the ³He/⁴He of air, 1.39 × 10⁻⁶), provides proxies to identify the participation of abiotic gases from the mantle or continental crust after eliminating the contribution of the atmosphere by referring to ⁴He/²⁰Ne ratio (Figure 8) (Graham, 2002). High R/Ra and high ⁴He/²⁰Ne ratios are the indication of the input of mantle-derived gases (Figure 8) (Oxburgh et al., 1986; Poreda et al., 1986).

FIGURE 8

Figure 8 Compiled of published noble gases geochemical data of hydrate associated gases plotted in He isotope versus ⁴He/²⁰Ne ratio.

The content and isotope ratios of noble gases in hydrate-bearing sediments from the Haskon Mosby Mud Volcano reveal that all the samples are with non-atmospheric He, which is considered to be crustal/radiogenic origin, and transported to hydrate stability zone through mud volcano (Figure 8) (Prasolov et al., 1999). One of these sites is with higher isotopic ³He/⁴He ratio, which probably contains the contribution from mantle. The ³He/⁴He ratio of hydrate-associated venting gas in Sea of Marmara is as high as 5.25 Ra (Figure 8) (Ruffine et al., 2018), and similar high ³He/⁴He ratio was also found in the southern part of the Ganos fault in the same area (Burnard et al., 2012), indicating a possible mantle contribution through large-scale fault systems (Gautheron and Moreira, 2002). Snyder et al. (2020) reported noble gas results from gas hydrate in the Japan sea and found that hydrate gas is mainly of a mixture of thermogenic/crustal source, biogenic gases and mantle source. The existence of hydrate with mantle ³He/⁴He characteristics indicates that fluids enriched in mantle gases are the main cause of the mobilization of thermogenic gas in the active chimney structures of the Japan Sea (Figure 8).

5.3.3 Unresolved questions

Fractionation of noble gases during the hydrate formation, combined with the episodic cycle of hydrate melting and refreezing, complicated the scenarios for noble gases studies associated with gas hydrate. For example, high ³He/⁴He ratios, which are generally related to mantle source gas, are found in hydrate-associated gases which were determined as biogenic origin by δ¹³C_-CH4 in samples from Sea of Japan. However, low ³He/⁴He ratios are observed in hydrate-associated gases with thermogenic carbon isotope signature (Snyder et al., 2020). The authors proposed that hydrates which were formed from thermogenic gas in chimney experienced decomposition and reformation, and helium was lost in this process because it is difficult to be encaged in hydrate by its small molecular size (Snyder et al., 2020). Therefore, the melting and reprecipitation effect of gas hydrate may prevent the identification of the magmatic or radiogenic contribution.

Air contamination and gas-water interactions in the pretreatment process prevent accurate measurement of noble gases degassing from hydrate-bearing pressurized core, Moore et al. (2020) proposed the modified quantitative degassing method which can minimize these effects and applied this technique to samples from the Gulf of Mexico (Figure 8), which may be important for future hydrate-associated noble gases study. Although this modified method reduces the impact of air pollution, it still requires complex procedures and large sample quantity, so it is still in need of a better pre-treatment scheme for noble gas detection.

6 Conclusion

Many natural gas hydrate samples have been collected and studied through multiple approaches during the past decades. Based on the data published, the factors affecting the geochemical characteristics of hydrate-associated gases have been summarized, and the methods for identifying gas origins and delineating the post-generation processes have been reviewed.

1. Apart from the gas of abiotic origin, most of the hydrate-associated gases are derived from the degradation of organic matter. Different types of organic matter are with distinct hydrocarbon-generation profile in the course of thermal evolution, as indicated by the molecular and isotopic compositions of their products. Oil-type gas and coal-type gas are the products of different types of organic matter, while microbial gases and thermogenic gases are the product in different evolution stages of organic matter in the burial history of sediments.

2. The characteristics of hydrate-associated gases are affected not only by the primary properties of organic materials such as organic type and thermal maturity but also associated with the secondary processes in gas accumulation processes after generation. Among the secondary processes, migration, mixing and biodegradation are common in hydrate-bearing area.

3. Clumped isotopes with equilibrium signals can be a robust proxy to estimate the formation temperature of methane, whereas the data without equilibrium signals can reflect the secondary processes that lead to the deviation from the equilibrium state. Most published methane clumped isotopes from marine sediments are found locating in a reasonable temperature zone which are generally consistent to their surroundings.

4. Noble gases can play an important role in recognizing the dynamics of thermogenic hydrocarbon generation generated by interactions between hydrothermal fluids and deeply buried organic matter. As such, noble gas helium isotopic signatures provide an indicator of large-scale deep migration pathways.

Author contributions

Conceptualization, HL; writing—original draft preparation, YL; writing—review and editing, CJ and HL; supervision, HL; funding acquisition, HL. All authors have read and agreed to the published version of the manuscript.

Funding

This work was supported by China Geological Survey (No. DD20221703).

Acknowledgments

We would like to express our gratitude to researchers who focus on the gas geochemical characteristics of natural gas hydrate, their previous work laid the foundation of this review. We also appreciate the efforts of the editors and reviewers, who gave constructive comments and suggestions which greatly improved this manuscript and inspired in-depth discussion.

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

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Supplementary material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/fmars.2022.968647/full#supplementary-material

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