A Review of Biogenic Coalbed Methane Experimental Studies in China
Abstract
:1. Introduction
2. Progress in Techniques and Methods
2.1. Geochemical Technologies
2.1.1. Gas Chromatography
2.1.2. Isotope Analysis
- (1)
- Hydrogen isotope analysis of monomeric hydrocarbons. This technique mainly uses chromatography mass spectrometry to perform the online analysis of monomeric hydrogen isotopes. It is mainly used to investigate the effect of cracking temperature on the analysis of monomeric hydrocarbon hydrogen isotopes [9,15]. Monomeric hydrogen isotope analysis has made a substantial leap forward in the analysis of hydrogen isotopes, which is important for studying the maturity, origin and formation environment of natural gas, and it also creates the conditions for an in-depth understanding for analyzing the internal microstructure and fractionation process of stable isotopes in nature [13].
- (2)
- Carbon isotope kinetic technique. Carbon isotope kinetic simulation studies can simulate the evolution of stable carbon isotopes and effectively relate this to the sedimentary and thermal history of a basin to dynamically reproduce the formation of natural gas and fractionation of the carbon isotopes [9,16]. Its advantages make it important for identifying gas genesis types and gas sources. Furthermore, it is not only useful for screening primary or secondary gas, but also for predicting the nature and composition of reservoir gas and addressing other related issues.
- (3)
- Biomarker carbon isotope analysis. It was found that the carbon isotopes of biomarkers contain rich biological, geological, and geochemical information, and it is important to study the carbon isotopes within organic compounds [17]. The development of gas/liquid chromatography coupled with stable isotope mass spectrometry has allowed biomarker detection to evolve from simple content analysis to stable isotope analysis of a single compound [18]. Biomarker carbon isotope analysis can establish the connection between biological precursors and their products during diagenesis through structural inheritance and carbon isotope composition characteristics of the monomeric compounds, which can not only explain multiple genesis pathways of the same biomarker compound, but also record the environmental information at the time of organic matter production, as well as the transformation characteristics during degradation, thereby revealing the complex geochemical processes [13,19].
2.2. Methods and Means of Products in Biological CBM Simulation Experiments
- (1)
- Gas composition determination. For the characterization of gas components produced during the anaerobic fermentation of coal, the composition of the gas mixture is generally examined using gas chromatography.
- (2)
- Liquid Phase Testing. This technique includes detection of the liquid phase organic and inorganic ions. Gas chromatography-mass spectrometry is generally used to determine the content of volatile organic compounds [20]. For some large-molecule organic compounds that are difficult to volatilize, such as pyruvic acid and polycyclic aromatic hydrocarbons, the more efficient liquid chromatography-mass spectrometer is required [21]. Two methods are generally used for inorganic ion testing: ion chromatography and chemical methods. In addition to detecting anions, ion chromatography is also widely used in the detection of inorganic cations, such as , and [22].
- (3)
- Solid Phase Testing. The solid phase test includes the analysis of components, structure, morphology, functional groups, surface elements, and pores of coal. Physical analysis is often performed on coal according to the national standards for industrial, elemental, specular group reflectance, and maceral components. The structure of coal is generally analyzed using X-ray diffraction with Raman spectroscopy. X-ray diffraction analysis is an effective tool to study the crystal structure and material structure in coal and kerogen [23]. Raman spectroscopy can analyze the changes in single chemical bonds within the structure of coal crystals, as well as the vibrations of groups [24]. Coal morphology and bacteria on the coal surface can be observed by light microscopy, scanning electron microscopy, and atomic force microscopy [9]. Fourier transform infrared spectroscopy is generally used to analyze the structure of coal functional groups during methane production by microbial fermentation. X-ray photoelectron spectroscopy is used to understand the composition and state of elements on the coal surface, which can provide important information about the elemental species, chemical composition, and related electronic structure on the surface of coal samples [25]. The current parameters used to study the coal body pore structure are pore size, pore shape, and pore surface complexity, and the associated testing methods include gas adsorption operation, mercury intrusion porosimetry, microcomputed tomography, and small angle X-ray scattering [26].
2.3. Methods and Means of Microbial Community Analysis
3. Progress in Influencing Factors and Identification
3.1. Biogenic Coalbed Methane Identification
3.1.1. Identification of Gas Composition
3.1.2. Identification of Isotopic Composition
3.1.3. Biomarker Compound Identification
3.2. Influencing Factors of Biogenic Gas Generation in Coal Seam
3.2.1. Effect of Coal Reservoirs on Gas Production
- (1)
- Organic matter abundance. Organic matter is the material basis for biogenic CBM generation. The higher the abundance of organic matter, the more favorable the biogenic CBM generation. The total organic carbon (TOC) abundance can reflect the organic matter abundance in hydrocarbon source rock to some extent [70] (Table 2). Generally speaking, the higher the TOC, the easier it is to generate biogas. For example, the TOC content of hydrocarbon source rock in the southern Junggar Basin of China is 0.54~1.42%, and the TOC content of hydrocarbon source rock in the Dongying Formation of the Bohai Bay Basin is 0.3~5% [43]. Related studies have shown that atmospheric fields can be formed with a low organic carbon content under high deposition rates and large deposition thicknesses. Huang et al. [71] studied the biogenic gas characteristics of the Yinggehai Basin and showed that the average organic carbon content in source rocks where organic matter is present is about 0.4%, and that the basin is in an active biogenic gas generation stage. The average organic carbon content is 0.3% in the Quaternary lacustrine mudstone of the Qaidam Basin, which also forms an atmospheric field [72]. It has been shown that the thickness of the organic matter in gas source rocks can compensate for the limitation of organic matter abundance to some extent. For example, the existence of thick hydrocarbon source rock in the Norbei basin of the Sanhu depression in China compensates for the low TOC fraction, forming biogenic gas reservoirs with great potential [73,74]. Li [75] studied the abundance of soluble organic matter within hydrocarbon source rocks in the Sanhu area of the Qaidam Basin and found that the abundance of soluble organic matter in the Neoproterozoic–Quaternary strata is much greater than the conventional TOC detection value, which is significant for the evaluation of biogenic CBM resources. Obviously, the higher the organic matter abundance, the more favorable the bio-methane output. It is also worth noting that the evaluation index for organic matter abundance is an important evaluation criterion for biomethane generation, but it is not a decisive factor for evaluating the gas volume of biomethane reservoirs in a region.
- (2)
- Type of organic matter. The organic matter type is closely related to the production of biogenic CBM. Different types of organic matter have different properties and are used by microorganisms with different degrees of ease. Among the organic matter types used to generate biogenic gas, humic parent material in coal is the most easily degraded by microorganisms [76]. Semi-humic and herbaceous humic organic matter can provide the carbohydrates, such as cellulose, hemicellulose, sugars, and starch, needed for microbial metabolism, which promotes biogenic CBM production [54]. Hydrogen-rich, oxygen-rich organic matter also facilitates the production of biogenic CBM. Wang et al. [77] studied the Lu Liang Basin and found rich organic matter, and discovered that the organic matter composition of its Neoproterozoic gas source rock contains more type II casein, which is rich in protein and lipid-like compounds and has great potential for biogenic CBM. Zhang et al. [78] found that the biogenic gas reservoirs of the Sanjiang Basin are also dominated by type II organic matter. Meanwhile, many scholars have studied the hydrocarbon generation capacity of maceral components and found that different maceral components have different hydrocarbon generation capacities. Liu et al. [79] made a systematic study of the gas production characteristics of different maceral and their effect on gas production using thermal simulation experiments, showing that the main gas-producing microfractions were vitrinite and the exinite. Furthermore, with the increase in temperature, the ability of vitrinite to produce methane was higher than that of exinite, while the gas production rate of fusinite was very low. As shown in Figure 3 [80,81], our scholars selected lignite, long flame coal, gas coal, and fat coal produced from LiangJia coal mines, YiMa coal mines, DaTong coal mines, and PanYi coal mines as experimental samples, and found that the main maceral components of gas production were vitrinite/huminite in the biogenic CBM simulation output experiments, while the highest gas production was found in vitrinite/huminite in coal, followed by raw coal, and the lowest production was in exinite/liptinite.
- (3)
- Organic matter maturity. Organic matter maturity determines the biogenic CBM production to some extent (Table 3). It was found that low-rank coal is easier to degrade and produce methane than high-rank coal. The maturity of organic matter in the biogenic gas source rock is generally in the immature-low maturity stage (Ro < 0.4%) [74,78,82] with a low degree of condensation of organic matter aromatic nuclei. Furthermore, its molecular structure contains a large number of branched chains and oxygen-containing functional groups, and the pore structure of the coal sample is easily changed after biodegradation, which is conducive to biological enzyme activity on macromolecules and, thus, it is easily degraded by microorganisms [83]. Guo et al. [84] found that the organic matter content of low rank coal slurry is higher and that the aliphatic structure, hydroxyl, and amino groups in the coal are easily shed, which promotes microbial degradation. Biogas reservoirs have been formed in basins where the organic matter maturity of the biogas source rock is at the immature–low maturity stage, such as that observed in the Yinggehai Basin [85], the Qidong area of the Yangtze River Delta [86], and the Norbei area [73] in China.
3.2.2. Effect of Coal Reservoir Environment on Gas Production
- (1)
- Temperature. The right temperature will encourage microorganisms to perform at optimum efficiency, maximizing methane production. Through anaerobic coal fermentation experiments at different temperatures, domestic scholars have concluded that the methane yield is largest in the range of 303 K to 328 K, and the biomethane yield increases with increasing temperature within a certain range [88,89,90]. However, further research is needed to study the effect of temperature in a narrower range on the biomethane production. The optimum temperature for anaerobic fermentation of indoor coal is now generally considered to be 308 K [91]. Meanwhile, Tang et al. [92] found that at 338 K, the biomethane production mode was dominated by the acetic acid decomposition type, whereas above 338 K, the biomethane production mode was dominated by the CO2 reduction type, indicating that temperature not only affects the activity of methanogenic archaea, but also affects the biomethane output mode.
- (2)
- Trace elements. Trace elements influence the microbial community, and thus methane production during anaerobic metabolism [93,94]. Xia et al. [95] found that the production of biogenic CBM is stimulated by trace elements. For example, the combination of Fe2+ and Ni2+ has a production-enhancing effect on biogenic CBM, which can shorten the gas production cycle, while the fugacity state of the trace elements in coal shift toward the direction of improving biological effectiveness. Su et al. [96] also found that iron, nickel and cobalt elements affect in situ microorganisms in coal seams, and that iron and nickel elements have a greater impact. Sun et al. [94] investigated the effect of trace elements on the microbial structure in anaerobic fermentation systems and showed that the effect of trace elements on bacterial communities was most prominent for the phyla Bacteroides, thick-walled Bacteroides and Helicobacter, which induced the enrichment of acetic acetotrophic methanogens while promoting the balance between hydrolytic acidification and methanation during anaerobic digestion. Huang et al. [97] found that Fe2+ could promote the synthesis of hydrogenase, thereby increasing gas production. The production of CBM can be stimulated by adding trace elements, the effects of which are different for different types of trace elements. The specific reaction mechanism needs to be further discussed.
- (3)
- Ph and oxidation-reduction potential (Eh). The activity, as well as the physiological and biochemical characteristics of microorganisms during anaerobic fermentation, is closely related to the pH, and either too high or too low pH will affect biomethane production [98,99,100]. Biogenic CBM simulation experiments using coal samples as a substrate showed that the CH4 output is better at pH 7~8, and both overly-acidic and alkaline environments cause the CH4 output to decrease. Biogenic CBM simulation experiments using seafloor sediments as a substrate showed that the effect of pH on CH4 output varies with the burial depth of the samples (Figure 4) [101,102]. Jin et al. [103] studied the characteristics of microbial community at different pH and showed that pH affects the activity of coal as well as the microbial metabolic processes. When studying the formation pathway of secondary biogenic gas in Huainan, Ding et al. [104] found that pH within 7.2~7.9 is a suitable range for anaerobic bacteria and methanogenic archaea. It has been suggested that the optimal pH for methanogenesis is within the medium–basic range [105]. The lower Eh are suitable for biogenic CBM generation. Using low-rank coal substrate from ShaQu mine and YiMa mine, it was concluded from simulated biogenic CBM production experiments that a lower Eh makes methanogenic archaea metabolically active, thereby promoting the maximum amount and mass fraction for methane production (Figure 5) [106,107].
- (4)
- Salinity. Salinity has an effect on biogenic CBM production and the activity of methanogenic archaea. Biogenic CBM simulation experiments using low-rank coal as a substrate showed that the activity of methanogenic archaea was restricted with increasing salinity, thereby inhibiting methane gas production, and the corresponding decrease in gas production became obvious with increasing salinity [101]. In contrast, biogenic CBM simulation experiments using seafloor sediments showed that the effect of salinity variation on CH4 production was not significant (Figure 6) [102]. Other studies have also shown that increasing salinity causes a decrease in methane production and a lower methane concentration generated by anaerobic coal fermentation, which is not conducive to biogenic CBM production [108,109].
- (5)
- Specific surface area and particle size. The specific surface area and particle size affect biomethane production to some extent (Figure 7). A smaller coal particle size and an larger specific surface area enable microorganisms to be in full contact with the coal surface, which contributes to higher biomethane production [98]. Guo et al. [110] conducted gas production experiments using subbituminous coal and found that gas production increased as the coal particle size decreased. In gas production experiments using lignite of different particle sizes, Wang et al. [111] found that the smaller the particle size, the easier it was to produce methane; however, when the particle size was less than 0.15 mm, the effect of particle size on gas production was no longer obvious.
3.2.3. Deposition Environment and Deposition Time
- (1)
- Sedimentary environment. Some scholars believe that the mode of formation for biogenic CBM is closely related to the sedimentary environment. The formation pathway for biogenic CBM is closely related to the depositional environment. Biomethane in the marine environment is formed mainly through the reduction of CO2 [112]. Biomethane in the freshwater environment is formed mainly by acetic acid fermentation [113]. It has also been suggested that the biogenic CBM formation mechanism does not depend entirely on the depositional environment, and that both pathways of formation can exist in both the marine and terrestrial environments [114]. By analyzing the carbon and hydrogen isotopic compositions of 31 gas samples from 10 biogenic gas reservoirs in China, Shen et al. [115] studied their formation pathways and reservoir characteristics and showed that the formation pathway of biogenic CBM under marine conditions was the typical CO2 reduction pathway with a heavy hydrogen isotopic composition, but the biogenic gas formed under terrestrial conditions was also mainly the CO2 reduction pathway. Therefore, the formation mode of biogas is closely related to, but not entirely dependent on, the sedimentary environment.
- (2)
- Deposition time. Biogenic CBM production is related to the deposition time and, for shallow biogenic CBM, methane increases with deposition time. It has been shown that in well-preserved strata, gas reservoirs with industrial value can be formed with the change in deposition time, even if the organic carbon content is very low [116]. Lin et al. [117,118] studied the Late Quaternary biogenic gas reservoir in the coastal plain of Hangzhou Bay, China, and found that the formation of this gas reservoir did not exceed 12,000 years, and that the total gas volume reached 2445.27 × 108 m3. Moreover, the formation in the Dafosi well field in the Ordos Basin, which produces biogenic gas from the coal seam, has undergone a very long period of intermittent deposition, allowing atmospheric precipitation to transport microorganisms into the coal seam and promote the generation of biogenic CBM in the area [119].
3.3. Microorganisms
3.3.1. Microbial Characteristics of Coal Reservoirs
3.3.2. Microbially-Enhanced Biogenic CBM Production
4. Conclusions
- (1)
- An improved understanding of the influencing factors during the process of anaerobic coal fermentation and the mechanism of CBM production has greatly facilitated the process of using geochemical methods to search for natural gas deposits (for example, carbon isotope analysis techniques for biomarker compounds and hydrogen isotope analysis techniques for monomeric hydrocarbons) to better serve the needs of natural gas exploration.
- (2)
- The characteristics of the microbial community in coal and the exploration of synergistic effects within the microbial community have led to the rapid development of microbial production-enhancing technologies, such as bioaugmentation and biostimulation, which not only enrich the current production-enhancing methods for biogenic CBM, but also greatly improves the gas production potential of small and medium-sized gas reservoirs in China. Thus, as an important replacement energy source for natural gas, biogenic CBM is expected to become one of the main clean energy sources for the next stage of national economic development.
- (3)
- Experiments simulating coal gas production demonstrate that chemical pretreatment of coal can effectively depolymerize the complex macromolecules in coal into smaller molecules, making the coal matrix more accessible to microorganisms and, thus, increasing the coal bioconversion rate. The chemical pretreatment of coal provides a new direction to shorten the gas production process of microbial coal degradation, and also facilitates the increased production of biogenic CBM, which can better promote CBM towards a diversified path.
- (4)
- In the context of the “carbon peak, carbon neutrality” strategy, underground coal gasification–carbon capture utilization and storage technologies is one of the essential ways to reduce carbon emissions. Among them, with respect to CBM, in addition to CO2 replacement of CBM to achieve increased production of CBM, the injection of CO2 into goafs and abandoned mines and the recycling of CO2 through CO2 methanation can not only achieve the clean utilization of residual coal, but also promote CO2 emission reduction, which is expected to achieve the strategic goal of “carbon peak and carbon neutrality” as soon as possible.
Author Contributions
Funding
Informed Consent Statement
Data Availability Statement
Conflicts of Interest
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Genetic Type | Tracer Indicators | Ro/% | ||||
---|---|---|---|---|---|---|
Isotopic Composition δ13C1(PDB), δD1(SMOW) | Component Ratio | |||||
Organic genesis | Biogenesis | Protobiogenic gas | δ13C1 < −55‰ | φC1/φC1–5 > 0.95 | ≤0.5 | |
Secondary biogenic gas | δ13C1 < −55‰ δD1: −250‰~−150‰ | φC1/φC1–5 > 0.95 | 0.3~1.5 | |||
Thermo-genesis | Primary thermogenesis | Thermal degradation gas | δ13C1: −46.2‰~−35.1‰ δD1: −247.3‰~−225.9‰ | φC1/φC1–n: 0.84~0.94 CDMI: 0~90.55% | 0.5~2.0 | |
Thermal cracking gas | δ13C1: −37.5‰~−29.6‰ δD1: >−200‰ | φC1/φC1+2 > 0.99 φC1/φC2 ≥ 3385 CDMI: ≤0.13% | >2~ 2.5 | |||
Secondary thermogenesis | The hydrocarbon isotopes of methane become even lighter | The drying coefficient increased further, but the CO2 content increased | >0.5 | |||
Mixed genesis | Gas mixture | δ13C1: −61.3‰~−50.7‰ δD1: −242.5‰~−219.4‰ δ13C2: −26.7‰~−15.9‰ Δδ13CC2–C1: 30.7‰~57.4‰ | φC1/φC1–n: 0.993~1.0 φC1/φC2: 188.6~2993.7 φCO2 < 2% CDMI: 0.64%~3.06% | >0.5 | ||
Inorganic genesis | Inorganic gas | The content of CO2 > 60%, CDMI > 90 |
Index | Excellent | Fine | Good | Medium | Poor | Non-Source Rock |
---|---|---|---|---|---|---|
TOC/% | >4.0 | 2.0~4.0 | 1.0~2.0 | 0.5~1.0 | 0.25~0.5 | <0.25 |
chloroform bitumen “A”/ppm | >4000 | 2000~4000 | 1000~2000 | 300~1000 | 100~300 | <100 |
Organic acid content/% | >2.0 | 1.0~2.0 | 0.5~1.0 | 0.2~0.2 | 0.1~0.2 | <0.1 |
Index | Immaturity | Low Mature | Mature | High Mature | Over Mature | |
---|---|---|---|---|---|---|
Ro (%) | <0.5 | 0.5~0.7 | 0.7~1.3 | 1.3~2.0 | >2.0 | |
Buried depth (km) | Present buried depth | <2~3 | <2~3.5 | <3~5.3 | <3.8~6.2 | |
Ancient burial depth | <2~3 | 2~3.5 | 3~5.3 | 3.8~6.2 | >5~6.2 | |
Paleogeotemperature (K) | Measured ground temperature | <323~363 | <333~388 | <355~443 | <373~467 | >403~467 |
homogenization temperature of fluid inclusions | <50~90 | 60~115 | 85~170 | 100~194 | >130~194 | |
apatite fission track | <50~90 | 60~115 | 85~170 | 100~194 | >130~194 | |
TTI | <3 | 3~20 | 20~160 | 160~600 | >600 | |
Thermal weightlessness of coal (%) | >20 | <5 | ||||
coal volatile (%) | >25~30 | <10 | ||||
Ultimate analysis | H/C atomic ratio | 0.75~0.85 | <0.6 | |||
O/C atomic ratio | <0.2~0.25 | <0.05 | ||||
Exinoid group | thermal alteration index | <2.5 | 2.5~3.5 | 3.5~4.5 | >4.5 | 5 |
color | faint yellow -yellow | yellow-yellowish-brown | Yellowish brown-brown | Dark brown-brownish black | black | |
Pyrogenation | Tmax (K) | <703 | 703~710 | 710~748 | 743~813 | >773 |
IH (mg/g) | 150~250 | <0.6 |
Genus | Substrate | Ref: | |
---|---|---|---|
Bacteria | |||
Proteobacteria | Syntrophus | long-chain fatty acid; aromatics; long chain alkane | [126] |
Rheinheimera | [127] | ||
Pseudomonas | [128] | ||
Acinetobacter | [129] | ||
Arcobacter | Citrate | [129] | |
Ferribacterium | aromatic hydrocarbon; naphthalene | [127] | |
Desulfofustis | [130] | ||
Desulfonema | |||
Aquamicrobium | polycyclic aromatic hydrocarbons | [131] | |
Achromobacter | saturation; aromatics; organic acids; amino acids; carbohydrates | [131] | |
Advenella | |||
Comamonas | |||
Thauera | |||
Desulfovibrio | carbohydrates; hydrocarbon; organic acids | [131] | |
Citrobacter | hydrocarbon | [131] | |
Stenotrophomonas | |||
Actinobacteria | Gordonia | dibenzothiophene | [96] |
Mycobacterium | |||
Rhodococcus | [129] | ||
Brevundimonas | [129] | ||
Cellulomonas | cellulolytic; poor water soluble organic compounds | [131] | |
Bacteroidetes | Bacteroides | carbohydrate; saccharides | [129] |
Petrimonas | organic acids and polymers | [131] | |
Prolixibacter | VFA | [96] | |
Proteiniphilum | protein; alcohols; saccharides | [96] | |
Sediminibacterium | |||
Macellibacteroides | |||
Firmicutes | Clostridium | starch; cellulose; chitin; xylan | [132] |
Acidoaminococcus | [133] | ||
Ruminococus | [130] | ||
Sporomusa | [128] | ||
Tissierella | aromatics; amino acid | [96] | |
Tyzzerella | macromolecular | [131] | |
Lachnoclostridium | cellulolytic | [131] | |
Anaerofilum | |||
Syntrophomonas | [134] | ||
Acetonema | [131] | ||
Dehalobacter | chlorinated aliphatic; aromatic compounds | [131] | |
Desulfitobacterium | [131] | ||
Synergistetes | Aminobacterium | amino acids | [131] |
Methanogen | |||
Hydrogenotrophic | Methanocorpusculum | H2/CO2 | [135] |
Methnolinea Methanoregula | [136] | ||
Methanosphaerula | |||
Methanothermus | |||
Methanocaldococcus | |||
Methanogenium | |||
Methanolacinia | |||
Methanopyrus | |||
Methanotorris | |||
Methanofollis | [131] | ||
Methanocalculus | |||
Methanocella | [137] | ||
Methanoculleus | [96] | ||
Methanobacterium | |||
Methanothermobacter | |||
Methanothermococcus | [138] | ||
Methanoplanus | [139] | ||
Aceticlasitic | Methanococcus | acetic acid H2/CO2 | [138] |
Methanosaeta | [134] | ||
Methanothrix | [96] | ||
Methanobrevibacter | |||
Methanomicrobium | |||
Methanolinea | |||
Methylotrophic | Methanosphaera | Methylamine; formic acid; methanol | [136] |
Methanomassiliicoccus | |||
Methermicoccus | |||
Halomethanococcus | |||
Methanosalsum | |||
Methanohalobium | |||
Methanohalophilus | |||
Methanococcoides | |||
Methanomethylovorans | [96] | ||
Methanolobus | |||
Methanosarcina | [134] | ||
Methanimicrococcus | [140] | ||
Methanofastidiosa | [141] |
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Chen, R.; Bao, Y.; Zhang, Y. A Review of Biogenic Coalbed Methane Experimental Studies in China. Microorganisms 2023, 11, 304. https://doi.org/10.3390/microorganisms11020304
Chen R, Bao Y, Zhang Y. A Review of Biogenic Coalbed Methane Experimental Studies in China. Microorganisms. 2023; 11(2):304. https://doi.org/10.3390/microorganisms11020304
Chicago/Turabian StyleChen, Run, Yunxia Bao, and Yajun Zhang. 2023. "A Review of Biogenic Coalbed Methane Experimental Studies in China" Microorganisms 11, no. 2: 304. https://doi.org/10.3390/microorganisms11020304
APA StyleChen, R., Bao, Y., & Zhang, Y. (2023). A Review of Biogenic Coalbed Methane Experimental Studies in China. Microorganisms, 11(2), 304. https://doi.org/10.3390/microorganisms11020304