Peixin Zhang1,2Minfang Yang3Zhongfeng Jiang1Kai Zhou4Xiaotao Xu5Huijuan Chen1Xuran Zhu1Yanghang Guo1Huajun Ye1Yuchan Zhang1
Longyi Shao2
Jing Lu2*- 1School of Municipal and Environmental Engineering, Henan University of Urban Construction, Pingdingshan, Henan, China
- 2State Key Laboratory of Coal Resources and Safe Mining, College of Geoscience and Surveying Engineering, China University of Mining and Technology, Beijing, China
- 3Research Institute of Petroleum Exploration and Development, PetroChina, Beijing, China
- 4State Key Laboratory of Hydroscience and Engineering, Department of Hydraulic Engineering, Tsinghua University, Beijing, China
- 5General Prospecting Institute of China National Administration of Coal Geology, Beijing, China
Wildfires are a major source of perturbations to the Earth’s system and have important implications for understanding long-term interactions between the global environment, climate, and organisms. In this study, current evidence for global warming, wildfires, and floral changes across the Permian-Triassic (P-T) and Triassic-Jurassic (T-J) transitions were reviewed, and their relationships were discussed. Available evidence suggests that global plant community turnover and the decline in plant diversity across the P-T and T-J boundaries were primarily driven by widespread wildfires. The Siberian Large Igneous Province and Central Atlantic Magmatic Province released large amounts of isotopically light CO2 into the atmospheric system, contributing to global warming and increased lightning activity. This ultimately led to an increase in the frequency and destructiveness of wildfires, which have significantly contributed to the deterioration of terrestrial ecosystems, the turnover of plant communities, and the decline in plant diversity. Furthermore, frequent wildfires also constitute an important link between land and ocean/lake crises. Large amounts of organic matter particles and nutrients from the weathering of bedrock after wildfires are transported to marine/lake systems through runoff, contributing to the eutrophication of surface water and the disappearance of aerobic organisms, as well as hindering the recovery of aquatic ecosystems. These wildfire feedback mechanisms provide an important reference point for environmental and climatic changes in the context of current global warming. Therefore, the interplay between global warming, wildfires, and biological changes and their feedback mechanisms needs to be fully considered when assessing current and future risks to the Earth’s surface systems.
1 Introduction
Increased global warming, a trend that has been a result of human activity since the mid-20th century, has already led to an increase in the frequency and severity of fire weather worldwide, increasing the risk of wildfires (Jones et al., 2020; Sharifi, 2022). Previous studies have shown that climate change will increase the risk of wildfires, with a global increase in average temperatures; frequency and intensity/extent of heatwaves, and regional increases in the duration, intensity and frequency of droughts, have the potential to influence fire weather, and thus increase the ignition potential of wildfires (Jones et al., 2020; Sharifi, 2022). The potential of wildfire occurrence is increasing at an unprecedented rate, possibly comparable to the rapid climatic changes affecting Earth’s ecosystems in its geological past.
Widespread wildfires have played an important role in the Earth’s system changes since the emergence of Silurian land plants, profoundly affecting the patterns and processes of global ecosystems (e.g., Glasspool, 2000; Scott, 2000; Glasspool et al., 2004; Glasspool et al., 2015; Lu et al., 2020; Glasspool and Gastaldo, 2022; Xu et al., 2022; Zhang et al., 2022; Zhang et al., 2023a). Changes in wildfire activity in Earth’s history can be identified in sediment records through variations in the by-products of plant combustion, such as charcoal fossils, fusinite, and polycyclic aromatic hydrocarbons (PAHs) (e.g., Glasspool, 2000; Glasspool et al., 2004; Shen et al., 2011; Glasspool et al., 2015; Lu et al., 2020; Song et al., 2020; Glasspool and Gastaldo, 2022; Song et al., 2022; Xu et al., 2022; Zhang et al., 2022; Jiao et al., 2023; Zhang et al., 2023a). The earliest wildfires (inferred from charcoal fossils) date back to the Silurian period (ca. 400 Ma) (Glasspool et al., 2004) and are consistent with the first records of terrestrial flora (Belcher and Claire, 2013). Therefore, the record of wildfire activity extends throughout Earth’s turbulent climate history, covering many large and small timespans of climate changes over geologic periods that have been accompanied by global fluctuations in O2, CO2, and temperature (Figures 1A–C), including four of the ‘Big Five’ mass extinctions (Figures 1D–F).
Figure 1 Global warming/climatic disturbance event occurrences and their relationship to: (A) Modelled atmospheric CO2 concentrations; (B) Modelled average global temperatures; (C) Modelled atmospheric oxygen concentrations (with uncertainty ranges (dotted line)) (modified from Lenton et al., 2018); (D) Inertinite abundance (bin mean) from fossil peat deposits (modified from Glasspool and Scott, 2010); (E, F) Macro-evolutionary rates of extinction of fossil marine invertebrate taxa, from the Paleobiology Database (modified from Blois et al., 2013 and Dal Corso et al., 2022). PAL, present atmospheric level; PTME, Permian-Triassic mass extinction; TJME, Triassic-Jurassic mass extinction; OSME, Ordovician-Silurian mass extinction; CPME, Cretaceous-Paleogene mass extinction; LOME, Late Devonian mass extinction.
The Permian-Triassic (P-T) and the Triassic-Jurassic (T-J) mass extinctions, the first and third largest biotic crises in the Phanerozoic, respectively (e.g., Alroy, 2014; Dal Corso et al., 2022), were accompanied by significant changes in global atmospheric composition, environment, climate, and flora (Shen et al., 2019; Wignall and Atkinson, 2020; Dal Corso et al., 2022; Shen et al., 2022b; Shen et al., 2023). Available evidence suggests that the mass extinction of terrestrial and marine life during these events were ultimately caused by the eruptions of the Siberian Large Igneous Province (SLIP) and Central Atlantic Magmatic Province (CAMP) (Wignall and Atkinson, 2020; Dal Corso et al., 2022), which was accompanied by a combination of massive releases of greenhouse gases and toxic gases (Fielding et al., 2019; Cui et al., 2021; Shen et al., 2022a; Zhang et al., 2022; Wu et al., 2023), rapid global warming (McElwain et al., 1999; Bonis et al., 2010; Schaller et al., 2011; Sun et al., 2012; Wu et al., 2021), negative carbon isotope excursions (CIEs) (Hesselbo et al., 2002; Shen et al., 2011; Kovács et al., 2020; Ruhl et al., 2020; Wu et al., 2020; Shen et al., 2022b), widespread wildfires (Belcher et al., 2010; Shen et al., 2011; Petersen and Lindström, 2012; Lu et al., 2020; Song et al., 2020; Song et al., 2022; Jiao et al., 2023), increased continental weathering (Cao et al., 2019; Lu et al., 2020; Shen et al., 2022b), and increased erosion (Biswas et al., 2020; van de Schootbrugge et al., 2020; Kaiho et al., 2021).
In this study, published records of terrestrial wildfires and floral changes across the P-T and T-J transitions were reviewed to assess potential relationships between SLIP and CAMP eruptions, global warming, wildfires, and floral extinction/turnover. This will provide deeper insight into the effects of contemporary environmental changes and the response mechanisms of the Earth’s ecosystems to these changes.
2 Floral changes across the Permian-Triassic transition
During the P-T transition interval, rapid extinctions/disappearances of terrestrial plant communities and catastrophic declines in plant diversity occurred across different geographic and climatic zones (e.g., Fielding et al., 2019; Chu et al., 2020; Feng et al., 2020; Gastaldo et al., 2020; Mays et al., 2020; Shu et al., 2022; Shao et al., 2023). This redefined the history of floral evolution, followed by the Early-Middle Triassic coal gap (the interval between the disappearance of coal-forming plants). Global coal-forming plants did not fully recover and form global coal deposits until the Late Triassic Carnian (e.g., Gastaldo et al., 1996; Dal Corso et al., 2020; Zhang et al., 2023b). Although some studies suggest that terrestrial plant loss was relatively milder compared to that of animals (Schneebeli-Hermann et al., 2017; Nowak et al., 2019), the abrupt halt in global peat formation represents a clear signal of significant terrestrial plant loss during the P-T transition (Gastaldo et al., 1996; Dal Corso et al., 2020).
In the high latitudes of the Southern Hemisphere, plant macro- and microfossils in Australia indicate the rapid transformation of Glossopteris flora into gymnosperms (lycopodium) and fern dominated flora during the P-T transition interval, and the subsequent loss of coal seam and rapid colonization of planktonic algae, fungi, and bacteria (Fielding et al., 2019; Mays et al., 2020; Vajda et al., 2020; Mays et al., 2021; McLoughlin et al., 2021). In the mid-latitudes of the Southern Hemisphere, plant communities from the Karoo Basin (inferred from plant macro- and microfossils) have undergone similar transformations, characterized by taeniate bisaccate Protohaploxypinus and Striatopodocarpidites pollen are replaced by assemblages rich in algal remains and low abundance of non-taeniate, alete bissacate pollen and cavate spores (Gastaldo et al., 2020), and the rapid increases followed by rapid deceases trend in the terrestrial plant index (the ratios of normal alkanes of terrestrial plant origin to total normal alkanes) from Guryul Ravine, India, indicates that the land plant community has also experienced catastrophic losses, characterized by a sharp reduction in the amount of terrestrial vegetation, occurred before and at the end-Permian marine extinction (Aftabuzzaman et al., 2021).
Near the equator, plant macrofossil records in South China show that terrestrial plants across the P-T transition led to the rapid disappearance of coal-forming plants such as lycopodium, ferns, seed ferns, and cycads in Cathaysia flora, with species reduction of 95% and genera reduction of 50% (Zhang et al., 2016; Chu et al., 2020; Feng et al., 2020). The latest palynological fossil results show the occurrence of two significant changes in the terrestrial plant community and plant diversity in South China across the P-T transition (Hua et al., 2023; Shao et al., 2023). The first was accompanied by a significant change of plant community dominated by Gigantopteris to gymnosperms, and the second was accompanied by a collapse of plant community and a significant decline in plant diversity (inferred from the disappearance of spores and pollen) (Hua et al., 2023; Shao et al., 2023). In addition, the change trends of land plant indices from South China (including Meishan, Shangsi, Liangfengya, Huangzhishan, and Xiaohebian sections) and Italy (Bulla Section) also show a catastrophic loss of land plant communities across the P-T transition (Biswas et al., 2020; Aftabuzzaman et al., 2021; Kaiho et al., 2021).
In the lower latitudes of the Northern Hemisphere, Cathaysia flora dominated by ferns and Gigantopteris gradually disappeared and was transformed into a Euramerican type Zechstein flora dominated by gymnosperms including conifers and pteridosperms (= seed ferns) in the lowest part of the Sunjiagou Formation (Wuchiapingian-Changxingian Stage transition) of the NCP (e.g., Wang and Chen, 2001; Yang and Wang, 2012; Lu et al., 2020). In the middle and/or upper part of the Sunjiagou Formation (Late Permian), plant macrofossil records show the disappearance of approximately 54% (14/26) of genera and approximately 88% (28/32) of species (Chu et al., 2015; Chu et al., 2019) and the interval of plant extinctions during the Early Triassic (Shu et al., 2022). Recent palynological results also indicate a catastrophic loss of terrestrial plant communities and plant diversity in the Yiyang coalfield of the NCP across the P-T transition (Zhang et al., 2023a). In the mid-latitudes of the Northern Hemisphere, the Junggar Basin in northwestern China has also experienced significant terrestrial flora and fauna loss across the P-T transition (Cao et al., 2008; Cai et al., 2021a). In the high latitudes of the Northern Hemisphere, plant macrofossils from Russia show a catastrophic loss of plant communities and plant diversity during this time interval (Krassilov and Karasev, 2009). In summary, the P-T transition experienced a catastrophic loss of terrestrial floras on a global scale.
3 Floral changes across the Triassic-Jurassic transition
During the T-J transition interval, the communities and diversity of terrestrial plants also showed significant changes across different geographic and climatic zones (e.g., Li et al., 2020; Zhang et al., 2022). This reflects another terrestrial plant diversity loss event after a period of complete recovery (the plant radiation during the Carnian Pluvial Episode of the Late Triassic) (Dal Corso et al., 2020; Lu et al., 2021; Zhang et al., 2023b) after the end-Permian terrestrial flora extinctions. This event also had an important impact on the global environment and climate change.
Studies on the western Tethys and Southern Hemisphere report the occurrence of a significant turnover of terrestrial plant communities and a decline in plant diversity across the T-J transition. In the western Tethys (including North America, Germany, Denmark, East Greenland, southwest England, and Austria), floral changes during the T-J transition interval occurred as follows: (1) an end-Triassic fern peak (including Polypodiisporites polymicroforatus, and trilete megaspores in some areas); (2) the first appearance of Cerbropollenites thiergartii and the last occurrence of Lunatisporites rhaeticus during the earliest Jurassic; and (3) a brief proliferation of Classopollis pollen (Cheirolepidiaceae) during the earliest Jurassic and the subsequent restoration and dominance of conifers (Olsen et al., 2002; Whiteside et al., 2007; Bonis et al., 2009; van de Schootbrugge et al., 2009; Bonis et al., 2010; Pieńkowski et al., 2012; Vajda et al., 2013; Lindström et al., 2017; Wignall and Atkinson, 2020; Boomer et al., 2021). Similarly, palynological fossil results from New Zealand and Australia in the Southern Hemisphere also show a significant turnover in terrestrial plant communities (De Jersey and McKellar, 2013). In New Zealand, terrestrial plants from the Late Triassic were dominated by lycophyte and bryophyte spores and corystosperm pollen, and those from the Early Jurassic were dominated by Osmundaceous spores and Classopollis pollen (Cheirolepidiacea) (De Jersey and McKellar, 2013). A similar pattern is observed in Australia, where terrestrial plants range from the Late Triassic dominated by ferns and bryophyte spores to the Early Jurassic dominated by Cheirolepidiacean pollen (De Jersey and McKellar, 2013).
Studies on the eastern Tethys also report a significant turnover of terrestrial plant communities and a decline in plant diversity across the T-J transition (Li et al., 2020; Zhou et al., 2021; Shen et al., 2022b; Zhang et al., 2022). In South China, plant macrofossil records (mainly pteridophytes) show a significant turnover of the terrestrial plant community; specifically, drought-resistant plant groups increased significantly across the T-J transition (Zhou et al., 2021). Similarly, palynological fossil results suggest species replacement of the terrestrial plant community, reflected by a change from predominantly pteridophyte lowland vegetation to coniferous species (Li et al., 2020). In North China, palynological fossil records show two significant changes in terrestrial plant communities and a decrease in plant diversity during this time interval (Zhang et al., 2022). In the first instance, the dominant gymnosperm pollen was replaced by algae and fern spores, and the proportion of palynological fossils decreased by ca. 45% (from 38 genera to 21 genera) (Zhang et al., 2022). In the second instance, the dominant fern spores were replaced by gymnosperm pollen, and the proportion of palynological fossils decreased by ca. 44% (from 50 genera to 28 genera) (Zhang et al., 2022). In northwestern China, both plant macro- and microfossils show that the rapid rise of fern spores, and the subsequent change from fern spores to gymnosperms occurred across the T-J transition (Lu and Deng, 2005; Shen et al., 2022b). In summary, terrestrial floras have experienced a significant global turnover of plant communities and a decrease in plant diversity across the T-J transition.
4 Contemporaneous wildfires linked to volcanism as a potential cause for floral changes
Contemporaneous widespread wildfires are believed to have been a major contributor to changes in the terrestrial environment, climate, and floras across the P-T and T-J transitions (Cao et al., 2008; Shen et al., 2011; Yan et al., 2019; Lu et al., 2020; Cai et al., 2021a; Cai et al., 2021b; Zhang et al., 2022; Zhang et al., 2023a) (Figures 2, 3). During the P-T and T-J transition intervals, published studies have shown that frequent wildfires are primarily controlled by their ignition mechanisms, namely the increased frequency and intensity of lightning activity, which is primarily associated with rapid increases in global temperatures (e.g., Glasspool et al., 2015; Lu et al., 2020; Zhang et al., 2022; Zhang et al., 2023a). Greenhouse warming (increased temperature), related to high CO2, resulted in an increase of upper-tropospheric water vapor, leading to more lightning activity and storminess (Miller and Baranyi, 2021). During the P-T and T-J transition intervals, SLIP and CAMP released large amounts of isotopically light CO2 into the atmospheric system, resulting in a significant increase in global temperatures and subsequent enhanced lightning activity (Glasspool et al., 2015; Miller and Baranyi, 2021), ultimately leading to an increase in wildfire frequency and destructiveness (van de Schootbrugge et al., 2008; Belcher et al., 2010; Glasspool et al., 2015; Lu et al., 2020; Zhang et al., 2022; Zhang et al., 2023a) (Figures 2, 3).
Figure 2 Global paleogeography during Permian-Triassic (A) and Triassic-Jurassic (B) transitions, including the location of the Large Igneous Province and wildfires around the world (modified from Lu et al., 2020; Vajda et al., 2020; Zhang et al., 2022; Zhang et al., 2023a). Wildfire distributions from Song et al. (2020), Song et al. (2022), Cai et al. (2021a), and Jiao et al. (2023). NCP, North China Plate; SCP, South China Plate; SLIP, Siberian Large Igneous Province; CAMP, Central Atlantic Magmatic Province.
Figure 3 Extinction mechanisms. (A, B), Summary of the volcanically triggered extinction mechanisms inferred from the geochemical, sedimentary, and paleontological record of the Permian-Triassic and Triassic-Jurassic mass extinctions and their recorded effects on biota in the ocean/lake.
Widespread wildfires across the P-T and T-J transitions caused the disappearance/extinction of terrestrial plants, marking significant changes in plant communities and diversity. During the P-T transition interval, evidence from charcoal, fusinite, and PAHs shows the prevalence of massive wildfires worldwide, including eastern Greenland (Nabbefeld et al., 2010), Brazil (Manfroi et al., 2015; Kauffmann et al., 2016), Australia (Glasspool, 2000; Vajda et al., 2020), India (Murthy et al., 2020), Canada (Nabbefeld et al., 2010; Grasby et al., 2011), South China (Shen et al., 2011; Zhang et al., 2016; Yan et al., 2019; Chu et al., 2020; Cai et al., 2021b; Song et al., 2022; Jiao et al., 2023), North China (Lu et al., 2020; Zhang et al., 2023a), and northwestern China (Cao et al., 2008; Cai et al., 2021a) (Figure 2A). During the T-J transition interval, evidence from charcoal, fusinites, and PAHs shows a global prevalence of large-scale wildfires, including North America (Jones et al., 2002), eastern Greenland (Belcher et al., 2010), Poland (Marynowski and Simoneit, 2009), Denmark (Lindström et al., 2019; Lindström et al., 2021), Sweden (Lindström et al., 2019; Lindström et al., 2021), South China (Pole et al., 2018; Song et al., 2020), and North China (Zhang et al., 2022) (Figure 2B). In addition, frequent wildfires during the aforementioned periods also had positive feedbacks on global warming and the carbon cycle because biomass burning also releases large amounts of isotopically light carbon into the atmosphere, further increasing the magnitude of global warming and CIEs (Ivany and Salawitch, 1993; Belcher et al., 2010).
Frequent wildfires also appear to be an important link between terrestrial and ocean/lake ecological crises. Widespread wildfire damage to surface vegetation can lead to the exposure of bedrock, leading to increased continental weathering, and increased soil erosion (e.g., Glasspool et al., 2015; Lu et al., 2020; Zhang et al., 2022) (Figure 3). These processes can release large amounts of organic matter (including charcoal and un-charred material) and nutrients (including phosphorus and potassium) into the ocean/lake system through surface runoff (Glasspool et al., 2015; Lu et al., 2020; Zhang et al., 2022) (Figure 3). These organic particles temporarily float in the ocean/lake, increasing ocean/lake turbidity through siltation and affecting light penetration and photosynthesis of marine/lake organisms (Glasspool et al., 2015) (Figure 3). Large nutrient inputs to the ocean/lake promote the eutrophication of surface water and the proliferation of cyanobacteria and algae (Liu et al., 2022) (Figure 3). In this context, oxygen circulation between ocean/lake surface water and the atmosphere will be suppressed by floating organic particles, cyanobacteria, and algae (Glasspool et al., 2015). The death of algal blooms reduces the amount of dissolved oxygen in water, produces toxic secondary metabolites (Mays et al., 2021), and enhances alkalinity in local micro-environment via a decaying hydrolytic destruction (Luo et al., 2021), impeding the recovery of ocean/lake ecosystems (Mays et al., 2021). These combined factors also further contribute to an anoxic environment in the ocean/lake and lead to the extinction of aerobic organisms.
The two examples discussed in this study highlight the interplay between wildfires and a wide range of environmental and climatic change processes in the Earth’s surface systems, which is critical to the complete understanding of the feedback effects of wildfires and their changes on terrestrial ecosystems over various time scales. In modern ecosystems, global warming and drought-induced climate conditions triggered by high levels of anthropogenic greenhouse gas emissions pose several risks to the Earth’s environment (Sharifi, 2022). In particular, these issues have the potential to increase the probability of widespread natural fires, which have a significant impact on plants, animals, and other natural resources worldwide (Sharifi, 2022). The interaction between fuel and climate and weather conditions determine fire regimes, driving the transformation of smoldering peat fires and low-intensity surface fires to intense crown fires. In turn, these fire regimes influence environmental and climatic change (including atmospheric concentration) over a range of short and long timescales through their feedbacks to geophysical and biological processes. For example, changes in vegetation types can affect wildfire types, and frequent terrestrial wildfires can in turn affect biological and geochemical processes in the Earth’s surface systems, such as nutrient transport, resulting in the loss of aerobic organisms in lakes and oceans (Glasspool et al., 2015; Zhang et al., 2022). Similarly, wildfires account for up to 20% of global greenhouse gas production and can travel at speeds of up to 22 km/h, indicating their potential for rapid devastation over large areas of land (Sharifi, 2022). Therefore, when assessing risks to modern and future surface system ecosystems, the interactions and feedback processes between wildfires, climate, and organisms on different time scales should be properly taken into account. An essential requirement for understanding potential future global warming-driven changes in the global fire regime and their impact over time is to clarify these feedback processes and the timescales over which they operate.
5 Conclusion
Studies of wildfires (inferred from charcoal fossils, fusinites, and PAHs) and plants (inferred from macro- and microfossils) across the P-T and T-J transitions have shown that widespread wildfires are the main drivers of the deterioration of terrestrial ecosystems, turnover of plant communities, and decline in plant diversity. SLIP and CAMP can release large amounts of greenhouse gases into the atmospheric system, contributing to global warming and an increase in the frequency of lightning activity, which ultimately enhance the frequency and destructive capacity of wildfires. Wildfires will affect the global environment through positive feedback effects. In other words, biomass burning will also release large amounts of isotopically light CO2 into the atmospheric system, further increasing the magnitude of global warming and CIEs. In addition, large amounts of organic particles and nutrients produced by the weathering of bedrock after wildfires are transported to lakes or marine systems through surface runoff, causing eutrophication of surface water and the disappearance of aerobic organisms, as well as hindering the recovery of aquatic ecosystems.
Author contributions
PZ: Writing – review & editing. MY: Writing – review & editing. ZJ: Writing – review & editing. KZ: Writing – review & editing. XX: Writing – review & editing. HC: Writing – review & editing. XZ: Writing – review & editing. YG: Writing – review & editing. HY: Writing – review & editing. YZ: Writing – review & editing, Validation. LS: Writing – review & editing. JL: Writing – original draft, Writing – review & editing.
Funding
The author(s) declare financial support was received for the research, authorship, and/or publication of this article. Financial support was provided by the National Natural Science Foundation of China (42172196, 41772161, and 41472131), the National Key Research and Development Program of China (2021YFC2902000), the Fund of Henan University of Urban Construction (K-Q2023019), and the National Science and Technology Major Project (2017ZX05009-002).
Conflict of interest
Author MY is employed by the company PetroChina and XX is employed by the company China National Administration of Coal Geology.
The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
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Keywords: Permian-Triassic transition, Triassic-Jurassic transition, global warming, widespread wildfires, floral change
Citation: Zhang P, Yang M, Jiang Z, Zhou K, Xu X, Chen H, Zhu X, Guo Y, Ye H, Zhang Y, Shao L and Lu J (2023) Significant floral changes across the Permian-Triassic and Triassic-Jurassic transitions induced by widespread wildfires. Front. Ecol. Evol. 11:1284482. doi: 10.3389/fevo.2023.1284482
Received: 28 August 2023; Accepted: 06 October 2023;
Published: 18 October 2023.
Edited by:
Dangpeng Xi, China University of Geosciences, ChinaReviewed by:
Mao Luo, Nanjing Institute of Geology and Paleontology (CAS), ChinaCopyright © 2023 Zhang, Yang, Jiang, Zhou, Xu, Chen, Zhu, Guo, Ye, Zhang, Shao and Lu. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Jing Lu, bHVqaW5nQGN1bXRiLmVkdS5jbg==