Jiye Li
Zhaofei Liu
Zhi Chen
Yan Gao1- 1Heilongjiang Earthquake Agency, Heilongjiang, China
- 2CEA Key Laboratory of Earthquake Prediction (Institute of Earthquake Forecasting), China Earthquake Administration, Beijing, China
- 3College of Transportation Engineering, Nanjing Tech University, Nanjing, China
Active fault zones are critical pathways for the migration of deep fluids to the Earth’s surface, carrying gases such as He, Rn, and CO2 that provide evidence for the physical and chemical dynamics of the Earth’s interior. This review examines the geochemical characteristics of fault zone gases and their implications for understanding fault activity and seismic events. Fault zones with high activity levels exhibit significant gas release, and variations in soil and hot spring gas concentrations can serve as indicators of seismic activity. Changes in gas concentrations and isotopic ratios, particularly before and after earthquakes, reflect the dynamic interplay between deep-sourced and shallow-sourced fluids. Seismic-induced stress alterations enhance gas release along fault zones, leading to observable anomalies that can aid in earthquake monitoring and prediction. The study underscores the importance of isotope tracing in deciphering fluid sources, migration pathways, and the evolution of fault zones, providing valuable information for assessing tectonic activity and mitigating seismic risks.
1 Introduction
Fluids play a crucial role in Earth’s system, particularly those migrating along fault zones, which often carry geochemical signatures indicating the physical and chemical evolution of Earth’s deep interior. These fluids serve as valuable indicators for studying block movements, earthquake prediction, fault activity assessment, and related fields (Martinelli, 2020; Zhang et al., 2021). Due to the high permeability and porosity of active faults, these zones frequently act as conduits for the migration and release of deep-sourced fluids. This process typically manifests at the surface through elevated soil gas emissions, including radon (Rn), carbon dioxide (CO2), helium (He), hydrogen (H2), and methane (CH4), as well as intense degassing from hot springs and increased geothermal heat flow (Weinlich, 2014; Voltattorni et al., 2015; Singh et al., 2016; Bond et al., 2017).
During fluid migration, stable isotope signatures of non-metallic elements frequently undergo equilibrium or kinetic fractionation. Isotopic analyses, such as 4He/20Ne, 3He/4He, and δ13CCO2, can elucidate the origins, migration pathways, circulation processes, formation mechanisms, and evolutionary history of these fluids (Zheng et al., 2013; Zhang et al., 2021). Furthermore, the chemical composition of fluids and isotopes is highly sensitive to variations in regional tectonic stress. Earthquake-induced stress changes can alter pore pressure and microcrack density, affecting fluid-rock interactions and subsequently modifying the surface emission levels of deep gases (Camarda et al., 2016; Randazzo et al., 2021; Caracausi et al., 2022). Therefore, analyzing the characteristics of fault zone gases and isotope sources provides an effective method for studying fluid migration within fault zones and its relationship to tectonic activity (Faulkner et al., 2010; Tian et al., 2021; Li et al., 2023).
2 Characteristics and sources of fluids in fault zones
2.1 Helium and neon
Helium (He) and neon (Ne) are inert noble gases whose isotopic compositions in various reservoirs make them effective geological tracers for mantle-derived fluids. Among the eight isotopic forms of helium, 3He and 4He are stable, while 5He through 10He are unstable. The ratios 4He/20Ne and 3He/4He are commonly employed to differentiate crustal from mantle-derived fluids (Sano and Wakita, 1985; Shao et al., 2024). The R/Ra ratio, representing He isotopic characteristics, is defined as the ratio of 3He/4He in a sample relative to that in the atmosphere.
In Earth’s atmosphere, He is predominantly composed of 4He, which constitutes ∼99.99986% of atmospheric He. The concentration of He in the atmosphere is relatively low, at 5.239 ± 0.004 ppm (Walia et al., 2010). The atmospheric 3He/4He (Ra) value is 1.4×10−6, and the 4He/20Ne value is ∼0.318 (Sano and Wakita, 1985). Most atmospheric 4He is radiogenic, originating from the α-decay of radioactive isotopes such as 238U, 235U, and 232Th (Figure 1). The He abundance in Earth’s crust is estimated at ∼ 5.5 × 10−7%. Crustal He typically exhibits an R/Ra value of ∼0.02 and a 4He/20Ne value of 1,000 (Andrews, 1985). Conversely, the 3He isotope, thought to originate from the solar nebula or solar wind radiation present during Earth’s formation, has accumulated in the mantle throughout Earth’s history. Mantle-derived He generally displays an R/Ra value exceeding 5 (Lupton, 1983), with mid-ocean ridge basalt (MORB) inclusions showing an R/Ra value of 8.0 and a 4He/20Ne value of 1,000 (Graham, 2002). R/Ra values between 5 and 50 are indicative of He from the lower mantle (White, 1957). The highest recorded R/Ra value of 67.2 ± 1.8 was found in olivine from 62 Ma-old lava flows on Baffin Island, suggesting a possible origin from Earth’s core (Horton et al., 2023). Due to He’s chemical inertness, stable physical properties, and low solubility in water, gases such as N2 and CO2, along with groundwater, often act as carriers for He migration (Hong et al., 2010; Walia et al., 2010; Lee et al., 2019). He typically accumulates in sedimentary basins and is released to the surface via faults or fractures (Gao et al., 2024).
Figure 1. The α-decay chains of 219Rn (A), 220Rn (B), and 222Rn (C), adapted from Soddy (1913) and Tan (2016).
2.2 Radon
Radon (Rn) is the only naturally occurring radioactive noble gas, existing in 34 unstable isotopic forms, ranging from 215Rn to 242Rn. In nature, radon is found primarily in three isotopes: 219Rn (with a half-life of 3.96 s), 220Rn (half-life of 55 s), and 222Rn (half-life of 3.82 days) (Audi et al., 2003). Of these, 222Rn is a decay product of 226Ra in the 238U decay chain (Figure 1), with the longest half-life, and its concentration in the atmosphere is typically ranging from 10 to 100 Bq·m-3 (Porstendörfer, 1994).
Uranium (U) and radium (Ra), naturally occurring radioactive elements, are widely distributed across the lithosphere, hydrosphere, and atmosphere. Uranium, which has 28 unstable isotopes (215U to 242U), is found in concentrations of ∼3 ×10−4% in the lithosphere and ∼1 × 10−4% in soil. Radium, with 33 unstable isotopes (202Ra to 234Ra), has lithospheric and soil concentrations of ∼1 × 10−4% and ∼8×10−11%, respectively (Cheng et al., 2005). The levels of U and Ra in soil or rock directly influence Rn release in soil gas (Pereira et al., 2017). Experimental studies on rock gas emissions have demonstrated that granite, which is rich in U and Ra, releases significantly higher Rn concentrations than limestone or sandstone (King, 1978; El-Arabi et al., 2006). Consequently, regions with extensive granite outcrops typically exhibit elevated Rn levels (Pereira et al., 2017).
Within mineral particles, radium undergoes α-decay, releasing α-particles (4He) and enabling Rn to escape. The fraction of Rn atoms generated from the decay of 226Ra that escape into rock pores is defined as the Rn emanation coefficient (Martinelli et al., 1995; Miklyaev et al., 2020; Phong Thu et al., 2020). Rn recoil can take three paths: 1) remaining within the same particle, 2) passing through a pore and embedding in adjacent particles, or 3) escaping into an open pore (Sakoda et al., 2011). Only Rn escaping into pore space is considered emanated (A, B, E, and F in Figure 2); otherwise, it is non-emanated (C, D, and G). The recoil range of Rn is 77 nm in water and 53 mm in the atmosphere, with the latter being 688 times greater (Sakoda et al., 2011). This difference indicates that rainfall and moisture content can significantly impact Rn diffusion.
Figure 2. A schematic of Rn atom α-recoil, adapted from Sakoda et al. (2011). Arrows indicate diffusion processes, and the carrier gas is illustrative and does not represent actual behavior. (A, B, E, F) represent Rn emanated; (C, D, G) are non-emanated.
Gas transport through porous media often occurs via two primary processes: diffusion and convection. Diffusion, driven by concentration gradients, involves the movement of substances from areas of high concentration to low concentration due to random molecular motion (Flügge and Zimens, 1939). Convection, also known as advection, mass transport, or viscous flow, is driven by pressure gradients (Ciotoli et al., 2007). In natural environments, gas transport typically results from a combination of these two mechanisms.
Due to Rn’s relatively large atomic mass and chemical inertness, deep-source gases such as CO2, N2, and CH4 often serve as carrier gases that facilitate its migration to the surface (Yuce et al., 2017). CO2, the most prevalent component of Earth’s interior, frequently acts as the carrier gas for Rn as it migrates along fault zones. Consequently, increased soil gas Rn concentrations are often observed in conjunction with rising CO2 levels in fault zones (Li et al., 2013). In rock fractures and pores, typically ranging from 10–2 to 101 mm in size at depths of several hundred to several thousand meters (Etiope and Martinelli, 2002; Girault and Perrier, 2014), Rn convection velocities can reach up to 100 to 104 m·d-1(Etiope and Martinelli, 2002; Muto et al., 2021). For example, convection velocities of Rn in the Osaka Basin, Baikal Rift, and North Caucasus are estimated at 340 m·d-1, 5.2 m·d-1, and 28 m·d-1, respectively (Miklyaev et al., 2020; Muto et al., 2021). When CO2 acts as the carrier gas, Rn may originate from depths of several hundred to several thousand meters in areas of high permeability (Girault and Perrier, 2014). Moreover, groundwater transport and deposition also contribute to the movement of Rn’s parent elements, uranium, and radium (Chen et al., 2018).
2.3 Carbon dioxide
Data from the Mauna Loa Observatory in Hawaii proves that the CO2 concentration in the atmosphere continues to increase, rising from 315.70 ppm in March 1958 to 422.80 ppm on 5 February 2024 (http://www.co2.earth). CO2 primarily originates from three sources: the decomposition of organic material, the breakdown of carbonate rocks, and mantle degassing (Barnes et al., 1978). The origin of CO2 can generally be determined using δ13CCO2 values and CO2 concentrations, which identify three distinct end-member sources: 1) Deep-source CO2, derived from magmatic degassing and the decarbonation of carbonate rocks, typically exhibits concentrations near 100% with δ13CCO2 values ∼0‰ (Parks et al., 2013); 2) Biogenic CO2, usually characterized by concentrations of ∼4% and δ13CCO2 values ∼ −23‰ (Di Martino et al., 2016); and 3) Atmospheric CO2, currently at 422.80 ppm, with δ13CCO2 values ∼ −8‰ (Keeling et al., 2005).
The range of δ13CCO2 from different sources can overlap each other, such as those from Mid-Ocean Ridge Basalts (MORB) and carbonate rocks (Bergfeld et al., 2001). CO2 also serves as the primary carrier gas for He migration in the crust (Hong et al., 2010; Walia et al., 2010; Lee et al., 2019). Therefore, the He-CO2 system is often utilized to further deduce the source of CO2 (Tian et al., 2021; Shao et al., 2024). Analysis of CO2 origins can be conducted using R/Ra ratios and δ13CCO2 values, which help distinguish between contributions from organic material, carbonate rock metamorphism, and mantle magma degassing (Barnes et al., 1978).
The decomposition of carbonate rocks involves processes such as water-rock interactions, mechanical grinding by faults, thermal metamorphism, and weathering (Rovira and Vallejo, 2008; Tamir et al., 2011). These processes can lead to the release of substantial amounts of CO2, which then becomes a crustal fluid, potentially contaminating mantle-derived volatiles. Typically, thermal metamorphism of carbonate rocks occurs ∼400°C; however, CO2 release can begin at temperatures above 70°C when water is involved (Pankina G et al., 1979). Extensive fracture networks and fluid interactions can enhance water-rock reactions within the rock, producing significant quantities of CO2 (Randazzo et al., 2021). Additionally, in regions of significant tectonic uplift, carbon stored in carbonate rocks for millions of years can be released through weathering (Zondervan et al., 2023).
3 Application of fault zone gases in tectonic activity
The Earth is an open system where fluids, especially gaseous components, play a crucial role in material and energy exchange across different layers. Active fault systems, characterized by higher permeability and porosity, facilitate the migration of deep-seated fluids (such as CO2 and He) toward the surface. These fault systems act as conduits extending to the mantle, allowing mantle-derived fluids to reach the Earth’s surface. The geochemical signatures of these fluids provide valuable insights into the physicochemical evolution of the Earth’s deep interior (Ciotoli et al., 2007; Yuce et al., 2017; Zhang et al., 2021), which constructed the major direction of gas geochemistry (Zheng et al., 2022). Therefore, in tectonically active regions, analyzing changes in fluid geochemical characteristics has become an essential method for studying block movements, earthquake prediction, revealing hidden faults, evaluating fault activity, and assessing atmospheric contributions (Zheng et al., 2018; Martinelli, 2020; Zhang et al., 2021).
3.1 Relationship between fault zone gases and tectonic activity
The exploration of soil gases, referred to as “geogas”, dates back to 1913 (Klusman, 1993). Globally, regions of strong gas release often overlap with tectonic suture zones, volcanic belts, geothermal areas, and seismic zones (Barnes et al., 1978; Tamburello et al., 2018). Regionally, the intensity of fluid release and the geochemical characteristics within fault zones are closely related to fault activity. Significant anomalies in soil gas concentrations (such as Rn, CO2, He, H2, and CH4) have been observed in various fault zones, including the Stivos Fault in Greece (Papastefanou, 2010), the Khlong Marui Fault in Thailand (Bhongsuwan et al., 2011), the Kütahya Simav Fault in Turkey (Manisa et al., 2022), and the Mat Fault in India (Jaishi et al., 2014). Field observations suggest that stronger fault activity correlates with increased soil gas release, making soil gas concentrations a useful metric for assessing fault activity (Seminsky et al., 2013; Capaccioni et al., 2015). Additionally, different fault types (normal, reverse, and strike-slip) exhibit distinct concentrations and flux characteristics (Annunziatellis et al., 2008; Sun et al., 2018). Therefore, tectonic zones with significant gas release are valuable for reconstructing regional geodynamic processes and monitoring subsurface tectonic activity (Faulkner et al., 2010; Tian et al., 2021; Li et al., 2023).
At a global scale, crustal permeability exhibits significant stratification, influenced by both internal and external forces. In the deeper crust, internal processes such as metamorphism and magmatism are dominant, while in the shallow crust, external factors, particularly the hydrologic cycle, play a more crucial role in shaping permeability (Rojstaczer et al., 2008). The difference in permeability of the crust determines the different distribution patterns of fluids underground. Rock deformation experiments indicate that when differential stress exceeds rock shear strength, pre-existing fractures close, forming new microcracks and pores. Continued stress can link these microcracks into macroscopic fractures, providing new pathways for fluid migration (Tuccimei et al., 2010). Under tectonic stress, the number of microcracks in fault zones increases (Li et al., 2013; Hansberry et al., 2021), accelerating the migration and release of deep gases, which can cause anomalies in gas concentrations and fluxes in shallow soils (Martinelli, 2020; Miklyaev et al., 2020). Research has shown that high sliding rates increase the permeability of sandstone and granite by three orders of magnitude, indicating that high sliding rates can sustain high permeability in fault zones (Tanikawa et al., 2010). Consequently, variations in soil gas release are primarily influenced by changes in fault zone permeability.
Active faults and fractures generally exhibit higher permeability and porosity than surrounding hard rock, resulting in greater deep-sourced gas release in fault zones compared to non-active tectonic areas (Annunziatellis et al., 2008; Giammanco et al., 2009; Weinlich, 2014; Voltattorni et al., 2015; Singh et al., 2016; Bond et al., 2017). In regions outside fault zones with lower permeability, the correlation between Rn and CO2 concentrations is weak. In contrast, well-connected faults show a stronger positive correlation between Rn and CO2 (Padrón et al., 2013; Ciotoli et al., 2014). Extensional structures with high permeability are more conducive to deep fluid release than thrust or strike-slip faults, with the scale of extensional faults directly influencing CO2 emissions (Tamburello et al., 2018). For example, CO2 emissions from the East African Rift are ∼71 Mt·yr-1 (Lee et al., 2016), from active rifts ∼40 Mt·yr-1 (Brune et al., 2017), and from the eastern Ethiopian Rift ∼20 Mt·yr-1 (Hunt et al., 2017) (Figure 3). Although active faults are key pathways for the release of mantle-derived and crust-derived gases (Caracausi et al., 2022), atmospheric gases can also enter the Earth’s interior through high-permeability fractures, with diffusion rates reaching 10 m·d-1 and maximum depths of 300 m (Arai et al., 2001; Giammanco et al., 2009). Additionally, thick sedimentary layers can obstruct gas migration, influencing atmospheric mixing and the release of deep-sourced gases, while shallow organic gases may mix with rising fluids (Liu, 2006). Therefore, the connectivity of fault zones significantly affects underground gas release, with surface gases reflecting a mix of various sources.
Figure 3. Comparison of the CO2 output in the arcuate structure zone and other regions of the world. Data from: the East African Rift (EAR) (Lee et al., 2016); the Tan-Lu Fault Belt, China (Aulbach et al., 2020); the Himalayas tectonic region (Becker et al., 2008); the present-day active rifts (Brune et al., 2017); the eastern Ethiopian rift (Hunt et al., 2017); the Mount Amiata, Italy (Sbrana et al., 2020); the Mineral spring, Slovakia (Kucharič et al., 2015); the Nyiragongo volcanoe, the East African Rift (Sawyer et al., 2008); the Oldoinyo Lengai volcanoe, the East African Rift (Brantley and Koepenick, 1995); the Icelandic geothermal systems (Ármannsson et al., 2005); the arcuate structure zone, the northeastern Tibetan Plateau (NETP) (Liu et al., 2024); the Magadi fault zone, the East African Rift (Lee et al., 2016); the western Ordos Basin, China (Liu et al., 2023a); the Wenchuan MS 8.0 earthquake rupture (Zhou et al., 2016); the Ustica volcanic island, Italy (Etiope et al., 1999); the Natron fault zone, the East African Rift (Lee et al., 2016); the Mount Changbai, China (Sun et al., 2021).
Deep and large active fault zones act as links across different Earth layers. Stable isotopes of deep fluids may undergo equilibrium or kinetic fractionation during geological processes, and fluid isotope tracers can provide important information on fluid sources and migration in active fault zones (Zheng et al., 2013; Zhang et al., 2021). For instance, (Hernández Perez et al., 2003) identified mantle-derived CO2 in soil gases of the Hakkoda Fault zone in northern Japan, with a contribution of up to 6.7%. Kulongoski et al. (2013) detected high 3He/4He ratios and CO2 concentrations in hot spring gases from the San Andreas Fault zone, with mantle-derived He contributing up to 44%. Shao et al. (2024) analyzed hot spring gases in the southern segment of the eastern boundary of the Sichuan-Yunnan rhombic block, finding no intersection between the Red River Fault and Xiaojiang Fault. Zhang et al. (2021) studied the southeastern margin of the Tibetan Plateau using the He-CO2-N2 system in hydrothermal fluids, finding that He isotopes provided evidence for the lateral expansion and localized surface uplift of the Tibetan Plateau. These studies demonstrate that surface-emitted gases and isotopes in hot springs or soil gases are effective indicators of tectonic activity and fluid dynamics.
3.2 Relationship between fault zone gases and seismic activity
Stress changes induced by earthquakes can trigger variations in pore pressure and the number of micro-cracks within fault zones, affecting the interaction between fluids and rocks and altering the release of deep gases at the surface (Camarda et al., 2016; Randazzo et al., 2021; Zhao et al., 2021; Caracausi et al., 2022). These processes can enhance fluid migration along active faults and modify the contribution of different fluid sources to soil gases and hot spring emissions, leading to observable pre-seismic anomalies or post-seismic responses (Martinelli and Dadomo, 2017). Between 1967 and 2014, analysis of 134 global seismic cases revealed that 69% showed anomalies in soil and groundwater Rn, 20% in geochemical parameters of soil and groundwater gases, and 10% in physical groundwater parameters (Woith, 2015) (Figure 4).
Figure 4. Global earthquake precursor statistics from 1967 to 2014, adapted from Woith (2015).
Recent studies have increasingly applied geochemical methods for analyzing soil gases to understand seismic activity trends and to develop earthquake monitoring and prediction theories. In tectonically active regions, stress accumulation from seismic activity enhances the release of deep-sourced gases like Rn, CO2, and He, which accumulate in rock fractures along fault zones (Ciotoli et al., 2014; Yuce et al., 2017; Chen et al., 2015). The correlation between Rn and CO2 concentrations tends to increase before earthquakes (Fu et al., 2017). The vibroseis truck (Gresse et al., 2016) and active seismic source (Liu et al., 2023b) experiments have demonstrated that seismic waves can boost the release of gases trapped in rock and soil pores. Moreover, low-magnitude earthquakes (M < 4) can release crustal He into the atmosphere, with the He release amount being quantitatively related to the fault zone volume (Caracausi et al., 2022). Periodic monitoring of soil gases in Italy’s Emilia region revealed significant increases in CO2, CH4, and H2 concentrations before and after the 2012 Emilia-Romagna earthquake swarm (Sciarra et al., 2017). In Gujarat, India, continuous Rn monitoring successfully detected significant increases in Rn concentrations days to weeks before four earthquakes with magnitudes ranging from 4.0 to 4.1 (Sahoo et al., 2020; Torkar et al., 2010) used soil gas Rn to predict 10 out of 13 earthquake events using an artificial neural network with a backpropagation algorithm. These findings highlight that seismic activity induces the release of deep-sourced gases along fault zones, leading to changes in soil gas concentrations that can serve as indicators for seismic activity and earthquake monitoring.
Hot spring gas geochemistry also shows potential as an indicator of seismic activity. Before the 2008 Tibet M 6.3 earthquake in China, significant anomalies in He and Rn concentrations were observed in hot springs at Bakreswar and Tatta Pani in India (Chaudhuri et al., 2011). Prior to the 1955 Kobe MW 6.9 earthquake in Japan, Rn release rates in groundwater and atmospheric Rn concentrations significantly increased, correlating with crustal strain fluctuations (Yasuoka et al., 2009). During the 2016 Kumamoto M 7.3 earthquake in Japan, He concentration changes in deep groundwater correlated with volumetric strain changes (Sano et al., 2016). Thus, hot spring gas concentrations can be crucial for earthquake monitoring.
Throughout different stages of earthquake preparation and occurrence, the contribution of deep-sourced and shallow-sourced fluids dynamically evolves. For instance, before and after the 2011 Van MW 7.2 earthquake in Turkey (Aydın et al., 2015) and the 2013 Lushan MS 7.0 earthquake in China (Chen et al., 2015), significant increases in 3He/4He and δ13CCO2 values were observed in hot spring gases in fault zones. As aftershock activity waned, the supply of mantle-derived gases decreased, leading to a decline in 3He/4He and δ13CCO2 values. Following the 2008 Iwate-Miyagi M 7.2 earthquake in Japan, the ascent of mantle-derived fluids caused a maximum 85% increase in the 3He/4He value in hot spring gases near the epicenter within a week (Horiguchi and Matsuda, 2008). After 2 M 6.0 earthquakes in the Emilia, Italy in 2012, the δ13CCO2 and δ13CCH4 values of gases released from fault zones in the epicentral area significantly decreased, likely due to the seismic-induced release of shallow biogenic CH4 and CO2, overshadowing deep thermogenic gases (Sciarra et al., 2017). These changes in He and C isotopes in hot spring gases near fault zones before and after earthquakes underscore how seismic activity promotes the mixing of gases from various sources, particularly the ascent of mantle-derived fluids.
Atmospheric gas variations induced by seismic activity are integral to understanding the lithosphere-atmosphere coupling mechanism (Veefkind et al., 2012; Jing et al., 2019). Advances in hyperspectral sensors with atmospheric detection capabilities have enabled extensive studies on gas changes associated with seismic and volcanic events (Tramutoli et al., 2013) (Figure 5). Notable anomalies in gases such as CH4, CO, CO2 and O3 have been documented before and after significant earthquakes, such as the 2004 Sumatra-Andaman MW 9.1 earthquake and the 2005 Sumatra-Nias MW 8.6 earthquake (Cui et al., 2023), the 2008 Wenchuan MS 8.0 earthquake and 2013 Lushan MS 7.0 earthquake in China (Cui et al., 2017), and the 2015 Gorkha M 7.8 earthquake and Dolakha M 7.3 earthquake in Nepal (Jing et al., 2019). Furthermore, a statistical analysis using the Adaboost machine learning algorithm examined infrared and hyperspectral gas parameters among 10 different variables before and after 1,371 global earthquakes of magnitude ≥6 from 2006 to 2013, identifying O3 and CO2 as significant contributors to earthquake prediction (Xiong et al., 2021).
Figure 5. Schematic diagram of satellite hyperspectral sensors and continuous monitoring station.
4 Conclusion
Active fault zones are vital conduits for deep fluids migrating to the Earth’s surface. The gases released (such as CO2, Rn, and He) contain valuable information about the physical and chemical evolution of the Earth’s interior and further reveal fault activity and seismic events. Isotope tracing is essential for identifying fluid sources, migration pathways, circulation processes, and formation mechanisms.
Gas release in fault zones is closely related to fault activity, and higher fault activity corresponds to higher soil gas release. Different fault types exhibit distinct geochemical fluid characteristics. Fault zones with strong gas release are preferred locations for studying regional geodynamics and monitoring subsurface tectonic activities.
Seismic activity alters stress states, which promotes the release of deep-sourced gases along fault zones and leads to anomalies in concentrations of soil gas and hot spring gas. These anomalies can serve as indicators of seismic activity, providing crucial information for earthquake monitoring. Isotopic changes in hot spring gases before and after earthquakes further demonstrate that seismic activity promotes the mixing of gases from different sources, especially the ascent of crustal or mantle-derived fluids.
In summary, fault zones are crucial for deep fluid migration and as research subjects for monitoring tectonic activity and earthquake prediction. Analyzing fault zone gas geochemistry enhances our understanding of the material cycle and energy exchange processes in the Earth’s interior, providing a scientific basis for disaster prevention and mitigation.
Author contributions
JL: Conceptualization, Data curation, Formal Analysis, Funding acquisition, Investigation, Methodology, Project administration, Resources, Software, Supervision, Validation, Visualization, Writing–original draft, Writing–review and editing. ZL: Conceptualization, Data curation, Formal Analysis, Funding acquisition, Investigation, Methodology, Project administration, Resources, Software, Supervision, Validation, Visualization, Writing–original draft, Writing–review and editing. ZC: Writing–original draft, Writing–review and editing. YG: Conceptualization, Data curation, Formal Analysis, Writing–original draft. YH: Conceptualization, Data curation, Formal Analysis, Writing–original draft. HG: Conceptualization, Data curation, Formal Analysis, Funding acquisition, Writing–original draft.
Funding
The author(s) declare that financial support was received for the research, authorship, and/or publication of this article. This work was supported by the National Natural Science Foundation of China (Grant No. 42372282) and the Science for Earthquake Resilience of China Earthquake Administration (Grant No. XH22035).
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.
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Keywords: gas emission, fault zone, fault activity, seismic activity, earthquake forecasting
Citation: Li J, Liu Z, Chen Z, Gao Y, Hao Y and Gu H (2024) The role of gas emissions (He, Rn, and CO2) from fault zones in understanding fault and seismic activity. Front. Earth Sci. 12:1488690. doi: 10.3389/feart.2024.1488690
Received: 30 August 2024; Accepted: 08 October 2024;
Published: 18 October 2024.
Edited by:
Fuqiong Huang, China Earthquake Networks Center, ChinaReviewed by:
Giovanni Martinelli, National Institute of Geophysics and Volcanology, ItalyGuodong Zheng, China University of Geosciences Wuhan, China
Copyright © 2024 Li, Liu, Chen, Gao, Hao and Gu. 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: Hongbiao Gu, aG9uZ2JpYW9zd0AxMjYuY29t