Skip to content


  • Full paper
  • Open Access

Kinetic effect of heating rate on the thermal maturity of carbonaceous material as an indicator of frictional heat during earthquakes

Earth, Planets and Space201870:92

  • Received: 31 March 2018
  • Accepted: 23 May 2018
  • Published:


Because the maximum temperature reached in the slip zone is significant information for understanding slip behaviors during an earthquake, the maturity of carbonaceous material (CM) is widely used as a proxy for detecting frictional heat recorded by fault rocks. The degree of maturation of CM is controlled not only by maximum temperature but also by the heating rate. Nevertheless, maximum slip zone temperature has been estimated previously by comparing the maturity of CM in natural fault rocks with that of synthetic products heated at rates of about 1 °C s−1, even though this rate is much lower than the actual heating rate during an earthquake. In this study, we investigated the kinetic effect of the heating rate on the CM maturation process by performing organochemical analyses of CM heated at slow (1 °C s−1) and fast (100 °C s−1) rates. The results clearly showed that a higher heating rate can inhibit the maturation reactions of CM; for example, extinction of aliphatic hydrocarbon chains occurred at 600 °C at a heating rate of 1 °C s−1 and at 900 °C at a heating rate of 100 °C s−1. However, shear-enhanced mechanochemical effects can also promote CM maturation reactions and may offset the effect of a high heating rate. We should thus consider simultaneously the effects of both heating rate and mechanochemistry on CM maturation to establish CM as a more rigorous proxy for frictional heat recorded by fault rocks and for estimating slip behaviors during earthquake.
Graphical Abstract image


  • Carbonaceous material
  • IR spectrometry
  • Raman spectrometry
  • Pyrolysis
  • Frictional heat
  • Heating rate


Frictional heat generated in fault zones constitutes the largest part of the total seismic energy budget during an earthquake (e.g., Chester et al. 2005), and it triggers several kinds of fault-weakening mechanisms, including thermal pressurization (Sibson 1973) and melt lubrication (Hirose and Shimamoto 2005), which can strongly affect earthquake energetics and fault slip behaviors. Because the progression of such mechanisms is closely dependent on the amount of heat produced by slip, to understand fault slip behaviors during earthquakes it is crucial to estimate the maximum temperature recorded by the fault rocks.

Several temperature proxies have been proposed as indicators of frictional heat recorded by fault rocks (Rowe and Griffith 2015). These include pseudotachylyte formation (e.g., Cowan 1999; Di Toro et al. 2005), mineral transformations (e.g., Hirono et al. 2007; Mishima et al. 2009; Kameda et al. 2011; Evans et al. 2014), thermal decomposition of carbonate minerals (e.g., Han et al. 2007; Oohashi et al. 2014), dehydration and dehydroxylation of clay minerals (e.g., Hirono et al. 2008; Schleicher et al. 2015), and anomalies in fluid-mobile trace element concentrations and strontium isotope ratios (e.g., Ishikawa et al. 2008; Honda et al. 2011). In particular, the thermal maturity of carbonaceous material (CM) has received considerable attention as a new temperature proxy (e.g., Savage et al. 2014; Hirono et al. 2015; Kaneki et al. 2016; Rabinowitz et al. 2017) because the organochemical characteristics of CM, including its elemental compositions and molecular structures, change irreversibly with increasing temperature (e.g., Beyssac et al. 2002). The frictional heat recorded by CM in both natural and experimental fault rocks has been investigated by spectroscopic analyses (e.g., Furuichi et al. 2015; Hirono et al. 2015; Kaneki et al. 2016, 2018; Ito et al. 2017; Kouketsu et al. 2017; Kuo et al. 2017) and by determining elemental compositions (Kaneki et al. 2016), biomarker indexes (Polissar et al. 2011; Savage et al. 2014; Sheppard et al. 2015; Rabinowitz et al. 2017), and vitrinite reflectance (e.g., O’Hara 2004; Sakaguchi et al. 2011; Kitamura et al. 2012; Maekawa et al. 2014; Hamada et al. 2015). Several studies have succeeded in inferring slip behaviors on natural faults during past earthquakes from estimations of maximum temperatures recorded by CM (Savage et al. 2014; Hirono et al. 2015; Kaneki et al. 2016; Mukoyoshi et al. 2018).

Maturation of CM is accompanied by the release of various volatile organic components (e.g., aliphatics, aromatics), resulting in the formation of a solid residue with extremely high carbon content (e.g., Spokas 2010). This devolatilization process can be strongly affected not only by maximum temperature but also by other factors such as a change in reactivity due to shear damage (mechanochemical effect) and the kinetic effect of the heating rate (e.g., Alexander et al. 1986; Kitamura et al. 2012). Recently, Kaneki et al. (2018) experimentally demonstrated that shear-enhanced mechanochemical effects can promote various organochemical reactions of CM at relatively low temperature and suggested that maximum temperatures estimated in the previous studies might be overestimated. Although it is known that higher heating rates generally lead to higher pyrolytic temperatures of CM (e.g., Alexander et al. 1986; Schenk et al. 1990; Huang and Otten 1998; Burnham and Braun 1999; Lievens et al. 2013), however, quantitative evaluation of the kinetic effect of heating rate on the CM maturation process during earthquakes remains unknown. Furthermore, several recent estimates of maximum temperatures are based on heating experiments conducted only at slow heating rates of about 1 °C s−1 (Hirono et al. 2015; Kaneki et al. 2016; Mukoyoshi et al. 2018). For example, Kaneki et al. (2016) inferred maximum temperatures and fault slip distances in the CM-bearing slip zone of an ancient plate-subduction fault developed in Kure Mélange, Shikoku, Japan (Fig. 1), to be 500–600 °C and 2–9 m, respectively, from the results of heating experiments on host-rock CM conducted using a heating rate of 50 °C min−1 (approximately 1 °C s−1). This rate is much lower than typical heating rates during earthquake slip (several tens to several hundreds of degrees per second); thus, these estimated temperatures and fault slip behaviors may include uncertainties due to the kinetic effect of heating rate.
Fig. 1
Fig. 1

Example of a CM-bearing fault. Location (upper) and photograph (lower) of an ancient plate-subduction fault developed in the Kure Mélange, Shikoku, Japan. The sampling point of CM-bearing non-deformed shale is shown by the black circle on the photograph of the outcrop. EUR Eurasia plate, NAM North American plate, PHS Philippine Sea plate

In this study, we quantitatively investigated the kinetic effect of heating rate on the thermal maturation of CM by using infrared (IR) and Raman spectrometry and pyrolysis–gas chromatography–mass spectrometry (py–GC/MS) in conjunction with slow- and fast-heating experiments. On the basis of our results, we show that the effect of heating rate on thermal maturation of CM has implications for the use of CM maturity as a proxy for frictional heat. We consider information about this effect to be crucial for establishing a more rigorous fault geothermometer and for estimating slip behaviors of past earthquakes.

Materials and methods

Heating experiments

To investigate the kinetic effect of heating rate on CM maturation, we collected CM-bearing bulk-rock samples from non-deformed shale in the Cretaceous Nonokawa Formation, in the Shimanto accretionary complex, which crops out along the coast at Kure, Tosa Town, Japan (Mukoyoshi et al. 2006) (Fig. 1). After extracting pure CM from the bulk samples by chemical treatment (HCl–HF method; see Kaneki et al. 2016 for details), we used a thermogravimetry–differential scanning calorimeter apparatus (STA 449 C Jupiter balance, Netzsch) for our slow-heating experiments. About 30 mg of the CM was placed in a covered Pt90Rh10 crucible and heated under Ar gas flow at a rate of 50 °C min−1 (approximately 1 °C s−1) from an initial temperature of 50 °C to target temperatures from 100 to 1000 °C at 100 °C intervals.

For the fast-heating experiments, we used a tube furnace to heat each CM sample. About 10 mg of sample was enclosed in a quartz tube (outer diameter, 8 mm; thickness, 1 mm; length, 25 cm) under vacuum (≤ 10 Pa), and then, the tube was inserted into the tube furnace apparatus, which had been preheated to the target temperature (100–1000 °C at 100 °C intervals), for 10 s. We numerically simulated the heating rates during the experiments by adopting a CM particle diameter of 100 µm (determined from scanning electron microscope observations) and thermal diffusivities of 1.6 × 10−7 and 8.7 × 10−7 m2 s−1 for CM and silica glass, respectively (Gustafsson et al. 1979; Turian et al. 1991). Then, we simulated the time–temperature and time–heating rate relationships for a CM particle with these thermophysical properties during the fast-heating experiments (Additional file 1). The simulated temperature profiles indicate that the heating rate increases as the target temperature increases, and the maximum heating rate that can be achieved is ≥ 100 °C s−1 for all target temperatures except 100 °C (for which 50 °C s−1 is the maximum rate) (Additional file 1). Hereafter, therefore, we refer to the slow- and fast-heating rates during the heating experiments as 1 and 100 °C s−1, respectively. We stopped the heating as soon as the targeted temperature was achieved.

Spectroscopic analyses

To investigate the chemical structures of CM, we conducted IR and Raman spectrometry on powdered CM samples. IR spectra of CM exhibit various peaks that correspond to organic and inorganic chemical bonds (e.g., Stuart 2004). These include an O–H stretching band at around 3400 cm−1; a sharp aromatic C–H band at 3050 cm−1; aliphatic hydrocarbon bands at 2960 cm−1 (asymmetrical CH3 stretching), 2930 cm−1 (asymmetrical CH2 stretching), and 2860 cm−1 (symmetrical CH2 stretching); a C=O stretching band at 1680 cm−1; an aromatic ring C=C stretching band at 1600 cm−1; and weak aliphatic hydrocarbon bending bands at 1455 cm−1 (asymmetrical CH3 bending) and 1375 cm−1 (symmetrical CH2 bending). We followed the methods of Kaneki et al. (2016) to obtain our IR spectra. We used a Fourier transform IR spectrometer (FT/IR-4700, Jasco Inc.) equipped with an IR microscope (IRT-5200, Jasco Inc.) to obtain IR absorbance spectra of CM retrieved from the shale and from the products of heating at 1 or 100 °C s−1. The samples were placed on a CaF2 plate and then hand-pressed to prevent saturation of the IR spectra. Before the measurements, plates and samples were dried in an oven at 50 °C for several hours. To acquire one IR spectrum, 100 spectra were accumulated with a wavenumber resolution of 4 cm−1, a wavenumber range of 4000–1000 cm−1, and an aperture size of 50 × 50 µm2. Background intensities of the IR spectra were eliminated by measuring a blank CaF2 plate.

Raman spectra of CM show significant peaks at 1355–1380 and 1575–1620 cm−1, which are known as disordered (D) and graphite (G) bands, respectively (Tuinstra and Koenig 1970). Several spectral parameters have been used to evaluate the maturity of CM in metamorphic rocks (e.g., Beyssac et al. 2002; Aoya et al. 2010; Kouketsu et al. 2014; Nakamura et al. 2015) and fault rocks (e.g., Hirono et al. 2015; Kaneki et al. 2016; Kouketsu et al. 2017; Kuo et al. 2017). We followed the methods of Kaneki et al. (2016) to acquire our Raman spectra and spectral parameters. We used a Raman microspectrometer (XploRA, Horiba Jobin–Yvon Inc.) equipped with a laser (532 nm) to obtain Raman spectra of CM powder derived from the shale and from the samples heated at 1 and 100 °C s−1. Before the measurements, samples were dried in an oven at 50 °C for several hours. Although the graphitic structure of CM has a crystallographic orientation (c-axis orientation), we did not control sample orientation during our spectral measurements because the orientation is unlikely to affect the Raman spectral features (Aoya et al. 2010). We used an exposure time of 10 s and a laser power of 0.09–0.11 mW to obtain spectra from the targeted surfaces to avoid thermal damage to the powder samples. Because Raman spectra obtained from the grain boundaries of CM particles might differ from those obtained from the body of CM particles (Tuinstra and Koenig 1970), we adopted a laser spot size of 5 µm as sufficiently smaller than the average CM particle size (approximately 100 µm). We then used PeakFit 3.0 software (Systat Software Inc.) to fit the D and G bands to the acquired spectra after a linear baseline correction of 1000–1800 cm−1 (Additional file 2). We determined the intensities of both bands. To compare the spectral features among the acquired Raman spectra, we normalized the spectra so that the height of the strongest peak of each spectrum was the same among the spectra being compared. Ten spectra were obtained from each sample (one spectrum per CM particle), and the mean values and standard deviations of the intensity ratios of the D and G bands (ID/IG) were calculated. All of the calculated ID/IG ratios with their standard deviations are summarized in Additional file 3.


To analyze the composition of gases released from the starting samples and from the samples that had been heated at 1 and 100 °C s−1, we followed the methods of Kaneki et al. (2016). We used a py–GC/MS system consisting of a model EGA/PY-3030D pyrolyzer (Frontier Lab) and a model GCMS-QP2010 SE GC/MS (Shimadzu) with an UltraALLOY-5 column. About 1 mg of sample was pyrolyzed at 1000 °C for 1 min under vacuum (≤ 2 Pa), and chromatographs and chemical compositions of the released gas were then analyzed. First, the intensities of the chromatographs were normalized by the weight of the analyzed samples, and then, the intensity ratios of toluene to benzene (Itoluene/Ibenzene) were determined. All of the calculated Itoluene/Ibenzene ratios are summarized in Additional file 3.


Spectroscopic characteristics

The IR spectra of CM from the shale (starting material) showed sharp absorbance peaks for the aliphatic C–H (2960, 2930, 2860, 1455, and 1375 cm−1), aromatic C–H (3050 cm−1), and C=C bonds (1600 cm−1) (Fig. 2). In the spectra of samples heated at 1 °C s−1, the absorbance peaks of the aliphatic C–H bonds and the aromatic C–H bond became weak at 600 °C and disappeared at 700 °C, and the absorbance peaks of the aromatic C=C bond became weak at 700 °C and disappeared at 800 °C (Fig. 2a). In the spectra of samples heated at 100 °C s−1, the absorbance peaks of the aliphatic C–H bonds and the aromatic C–H bond became weak at 800 °C and disappeared at 900 and 1000 °C, respectively, and the absorbance peaks of the aromatic C=C bond became weak at 900 °C and disappeared at 1000 °C (Fig. 2b).
Fig. 2
Fig. 2

Representative IR spectra of the analyzed CM. IR spectra of CM from shale and from products heated at a rate of a 1 °C s−1 or b 100 °C s−1. exp. experiment

The Raman spectra of all of the analyzed samples showed distinct D and G band peaks, and the intensity of the D band relative to that of the G band increased as the target temperature increased (Fig. 3). The ID/IG ratios of the samples heated at 1 °C s−1 increased markedly at ≥ 600 °C, whereas those of samples heated at 100 °C s−1 started to increase at ≥ 900 °C (Fig. 4).
Fig. 3
Fig. 3

Representative Raman spectra of the analyzed CM. Raman spectra of CM from shale and from products heated at a rate of a 1 °C s−1 or b 100 °C s−1. exp. experiment

Fig. 4
Fig. 4

Temperature dependence of the ID/IG ratios of the analyzed CM. Bars show standard deviations. exp. experiment


Chromatographs for the CM sample from shale and for the products of the heating experiments included clear peaks of various aromatic compounds, and the samples were especially rich in benzene and toluene (Fig. 5). The chromatographs for the products of the heating experiments showed a systematic decrease in peak intensities as the target temperature increased. Intensities of the benzene and toluene peaks of CM sample heated at 1 °C s−1 decreased markedly at 500 °C and approached zero at 700 °C (benzene) and 600 °C (toluene). In contrast, for the CM sample heated at 100 °C s−1, chromatograph peak intensities started to decrease at 800 °C and approached zero at 1000 °C. The Itoluene/Ibenzene ratios of the CM sample heated at 1 °C s−1 started to decrease at 500 °C, whereas the ratios of samples heated at 100 °C s−1 showed a sudden decrease above 800 °C. The Itoluene/Ibenzene ratios in samples heated at 1 °C s−1 to ≥ 700 °C and in those heated at 100 °C s−1 to 1000 °C could not be determined because of the extinction of the toluene and benzene peaks on those chromatographs.
Fig. 5
Fig. 5

Gas chromatographs of the analyzed CM. The two chromatographs at the top of each column show the composition of gas released from the starting CM. The lower 20 chromatographs show the compositions of gas released from the products heated at 1 °C s−1 (left column) and 100 °C s−1 (right column). exp. experiment

Discussion and conclusions

The py–GC/MS chromatographs revealed that the dominant components of the analyzed CM samples were benzene and toluene, and the amounts of these compounds decreased as the target temperature increased (Fig. 5). The presence of toluene or phenol, which have aliphatic C–H or O–H bonds in their molecular structures, clearly indicates that the CM from shale was not derived from C–H–O-rich fluid at high temperature (≥ 500 °C) because such depositional CM is almost fully graphitized (e.g., Luque et al. 2009). In samples heated at 1 and 100 °C s−1, the chromatographic peak of toluene disappeared (Fig. 5), and extinction of the aliphatic C–H absorbance peaks was observed on the IR spectra (Fig. 2), at 600 and 900 °C, respectively. This result clearly indicates that toluene dominantly controlled the amount of aliphatic C–H chain in the samples. Furthermore, the almost simultaneous disappearance of the chromatographic peak for benzene and the absorbance peak of the aromatic C=C bond at 700–800 and 1000 °C in the samples heated at 1 and 100 °C s−1, respectively (Figs. 2, 5), suggests that benzene was the main contributor to the aromatic C=C absorbance peaks on the IR spectra. The ID/IG ratios of the Raman spectra for the products heated at 1 and 100 °C s−1 began to increase at ≥ 600 and ≥ 900 °C, respectively (Fig. 4). This result is well consistent with the findings of several prior studies that showed ID/IG ratios increased when intact CM was exposed to high temperatures of several hundreds of degrees Celsius by heating or friction experiments (e.g., Furuichi et al. 2015; Hirono et al. 2015; Kaneki et al. 2016, 2018; Ito et al. 2017). In these temperature ranges, no significant change in the molecular compounds in gases released from the heating products was observed except for a small decrease in the chromatographic peak of benzene (Fig. 5). This result suggests that the changes in the ID/IG ratios are possibly attributable to pyrolysis of residual benzene with relatively strong bonds within the graphitic sheets accompanied by the formation of a disordered structure as a result of pyrolytic rearrangement. The abrupt decreases in the Itoluene/Ibenzene ratios at ≥ 500 and ≥ 800 °C in the products heated at 1 and 100 °C s−1, respectively, might be due to the difference in the pyrolytic temperatures of benzene and toluene (Fig. 6).
Fig. 6
Fig. 6

Temperature dependence of the Itoluene/Ibenzene ratios of the analyzed CM. The ratios of the products heated to ≥ 700 °C at 1 °C s−1 and to 1000 °C at 100 °C s−1 are not available owing to extinction of the toluene and benzene peaks. exp. experiment

On the basis of these results, we inferred that the dominant maturation process controlling the changes in the organochemical characteristics of the starting CM during the heating experiments was the thermal decomposition of benzene and toluene, which resulted in the extinction of absorbance peaks in the IR spectra at higher temperatures, and the subsequent rearrangement of residual aromatic nuclei, which in turn increased the ID/IG ratios of the Raman spectra. Although Kaneki et al. (2016) attributed changes in the characteristics of IR and Raman spectra of heated CM to the thermal decomposition of toluene and the growth of aromatic rings, our series of organochemical analyses, including py–GC/MS analyses, revealed that thermal decomposition not only of toluene but also of benzene, along with subsequent structural rearrangement that increased the ID/IG ratios, may have played a significant role in maturation process of our CM at high temperature.

Although our CM heating experiments were conducted under dry conditions, the in situ environment of natural fault rocks is usually water-saturated. Water saturation may affect the CM maturation process by providing an exogenous source of hydrogen (e.g., Lewan 1997). However, this hydrothermal effect is reported to appear only after a long reaction time of ≥ 70 h at temperatures of ≥ 330 °C (Lewan 1997). Because our heating experiments were completed within 20 min, we can ignore the effect of water saturation.

The ID/IG ratio of Raman spectra has long been believed to decrease with increasing CM maturity (e.g., Beyssac et al. 2002; Kuo et al. 2017), whereas we observed a completely opposite trend in our results (Fig. 4). However, recent friction and heating experiments conducted with pure CM or CM-bearing samples have demonstrated increases in the ID/IG ratios of CM with increasing temperature (e.g., Furuichi et al. 2015; Hirono et al. 2015; Kaneki et al. 2016, 2018; Ito et al. 2017). Furthermore, Mukoyoshi et al. (2018) reported an increase in the ID/IG ratios of CM in a natural pseudotachylyte-bearing slip zone relative to the ratios in host-rock samples. These contradictory results might be explained by heterogeneity of the initial condition of the CMs among these studies. For example, Kuo et al. (2017) obtained lower ID/IG ratios for anthracite samples in a high-velocity friction experiment, whereas Furuichi et al. (2015) reported an increase in the ID/IG ratios of brown coal in a similar friction experiment. If it is assumed that the direction of change in the ID/IG ratios of Raman spectra with increasing temperature depends on the initial maturity of the starting CM (e.g., Kouketsu et al. 2014, 2017; Schito et al. 2017), the increasing ID/IG ratios of the Raman spectra of CM with increasing temperature in our study might be attributable to the relatively low maturity of the starting CM (bituminous coal). Thus, to characterize fully the temperature–maturity relationship, further friction and heating experiments and organochemical analyses should be performed using CM samples with various initial maturities.

We obtained experimental evidence for the first time that a kinetic effect of heating rate is involved in various organochemical reactions of CM. The results of our organochemical analyses clearly indicate that a higher heating rate can inhibit various CM maturation reactions, including the thermal decomposition of several aromatic compounds and structural rearrangement, thus causing extinction of some IR spectral absorbance peaks, increases in the ID/IG ratios of Raman spectra, and decreases in the Itoluene/Ibenzene ratios on py–GC/MS chromatographs (Fig. 7). These results suggest that the maximum temperatures reported previously (Hirono et al. 2015; Kaneki et al. 2016; Mukoyoshi et al. 2018) might be too low. On the other hand, Kaneki et al. (2018) demonstrated that shear-induced mechanochemical effects can increase a reactivity of various organochemical reactions, thus lowering the temperatures necessary for the occurrence of CM maturation reactions by approximately 100 °C under a normal stress of 3 MPa and a slip distance of 10 m (Fig. 7). Although this study focused only on the kinetic effect of heating rate, to understand the CM maturation process during earthquake slip and to establish a more rigorous fault geothermometer based on CM maturity, these two, possibly opposite, effects should be considered simultaneously.
Fig. 7
Fig. 7

Summary of organochemical reactions of CM as a function of temperature. Quantitative data on the mechanochemical effect on reaction temperature are from Kaneki et al. (2018), who reported that the mechanochemical effect can cause CM maturation reactions to occur at temperatures approximately 100 °C lower under a normal stress of 3 MPa and a slip distance of 10 m. exp. experiment

In this study, we focused on how the heating rate might affect the maturation of CM during earthquake slip, and demonstrated experimentally that a high heating rate can inhibit various organochemical reactions of CM. Our results suggest that the maximum slip zone temperatures estimated previously by slow-rate CM heating experiments (Hirono et al. 2015; Kaneki et al. 2016; Mukoyoshi et al. 2018) might be underestimated. Furthermore, mechanochemical effects during earthquake slip can also strongly affect the maturation of CM (Kaneki et al. 2018). Therefore, comprehensive consideration of the effects on CM maturation of both heating rate and mechanochemistry, as well as of the initial maturity of the starting CM, is needed to establish a more rigorous proxy of frictional heat recorded in fault rocks and to infer fault slip behaviors during earthquakes.



carbonaceous material


Eurasia plate


intensity ratio of the D and G bands of Raman spectra



I toluene/Ibenzene

intensity ratio of the benzene and toluene peaks on gas chromatographs


North American plate


Philippine Sea plate


pyrolysis–gas chromatography–mass spectrometry


Authors’ contributions

Both authors designed the study. SK carried out all of the experiments, analyses, and numerical simulations. Both authors contributed to the interpretation of the results, collaborated in writing the early drafts. Both authors read and approved the final manuscript.


The authors thank Tadashi Kondo for help with our heating experiments. We are also grateful to Takuji Yamada for editing this paper and to Patrick Fulton and an anonymous reviewer for giving many constructive comments.

Competing interests

The authors declare that they have no competing interests.

Availability of data and materials

All data used in this study are available in the figures, additional files, and references. The data are also available from the corresponding author upon request.

Consent for publication

Not applicable.

Ethics approval and consent to participate

Not applicable.


SK was supported by a Grant-in-Aid for Japan Society for the Promotion of Science (JSPS) Fellows (KAKENHI No. 17J01607), and TH was supported by a Grant-in-Aid for Scientific Research (B) (KAKENHI No. 15H03737) from JSPS and by Grants-in-Aid for Scientific Research on Innovative Areas (Crustal Dynamics, KAKENHI No. 26109004) from the Ministry of Education, Culture, Sports, Science and Technology of Japan.

Publisher’s Note

Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (, which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

Authors’ Affiliations

Department of Earth and Space Science, Graduate School of Science, Osaka University, Toyonaka 560-0043, Japan


  1. Alexander R, Strachan MG, Kagi RI, van Bronswijk W (1986) Heating rate effects on aromatic maturity indicators. Org Geochem 10:997–1003. View ArticleGoogle Scholar
  2. Aoya M, Kouketsu Y, Endo S, Shimizu H, Mizukami T, Nakamura D, Wallis S (2010) Extending the applicability of the Raman carbonaceous-material geothermometer using data from contact metamorphic rocks. J Metamorph Geol 28:895–914. View ArticleGoogle Scholar
  3. Beyssac O, Goffé B, Chopin C, Rouzaud JN (2002) Raman spectra of carbonaceous material in metasediments: a new geothermometer. J Metamorphic Geol 20:859–871. View ArticleGoogle Scholar
  4. Burnham AK, Braun RL (1999) Global kinetic analysis of complex materials. Energy Fuels 13:1–22. View ArticleGoogle Scholar
  5. Chester JS, Chester FM, Kronenberg AK (2005) Fracture surface energy of the Punchbowl fault, San Andreas system. Nature 437:133–136. View ArticleGoogle Scholar
  6. Cowan DS (1999) Do faults preserve a record of seismic slip? A field geologist’s opinion. J Struct Geol 21:995–1001. View ArticleGoogle Scholar
  7. Di Toro G, Nielsen S, Pennacchioni G (2005) Earthquake rupture dynamics frozen in exhumed ancient faults. Nature 436:1009–1012. View ArticleGoogle Scholar
  8. Evans JP, Prante MR, Janecke SU, Ault AK, Newell DL (2014) Hot faults: iridescent slip surfaces with metallic luster document high-temperature ancient seismicity in the Wasatch fault zone, Utah, USA. Geology 42:623–626. View ArticleGoogle Scholar
  9. Furuichi H, Ujiie K, Kouketsu Y, Saito T, Tsutsumi A, Wallis S (2015) Vitrinite reflectance and Raman spectra of carbonaceous material as indicators of frictional heating on faults: constraints from friction experiments. Earth Planet Sci Lett 424:191–200. View ArticleGoogle Scholar
  10. Gustafsson SE, Karawacki E, Khan MN (1979) Transient hot-strip method for simultaneously measuring thermal conductivity and thermal diffusivity of solids and fluids. J Phys D Appl Phys 12:1411–1421View ArticleGoogle Scholar
  11. Hamada Y, Sakaguchi A, Tanikawa W, Yamaguchi A, Kameda J, Kimura G (2015) Estimation of slip rate and fault displacement during shallow earthquake rupture in the Nankai subduction zone. Earth Planets Space 67:39. View ArticleGoogle Scholar
  12. Han R, Shimamoto T, Hirose T, Ree JH, Ando J (2007) Ultralow friction of carbonate faults caused by thermal decomposition. Science 316:878–881. View ArticleGoogle Scholar
  13. Hirono T, Yokoyama T, Hamada Y, Tanikawa W, Mishima T, Ikehara M, Famin V, Tanimizu M, Lin W, Soh W, Song SR (2007) A chemical kinetic approach to estimate dynamic shear stress during the 1999 Taiwan Chi–Chi earthquake. Geophys Res Lett 34:L19308. View ArticleGoogle Scholar
  14. Hirono T, Fujimoto K, Yokoyama T, Hamada Y, Tanikawa W, Tadai O, Mishima T, Tanimizu M, Lin W, Soh W, Song SR (2008) Clay mineral reactions caused by frictional heating during an earthquake: an example from the Taiwan Chelungpu fault. Geophys Res Lett 35:L16303. View ArticleGoogle Scholar
  15. Hirono T, Maekawa Y, Yabuta H (2015) Investigation of the records of earthquake slip in carbonaceous materials from the Taiwan Chelungpu fault by means of infrared and Raman spectroscopies. Geochem Geophys Geosyst 16:1233–1253. View ArticleGoogle Scholar
  16. Hirose T, Shimamoto T (2005) Growth of molten zone as a mechanism of slip weakening of simulated faults in gabbro during frictional melting. J Geophys Res 110:B05202. Google Scholar
  17. Honda G, Ishikawa T, Hirono T, Mukoyoshi H (2011) Geochemical signals for determining the slip–weakening mechanism of an ancient megasplay fault in the Shimanto accretionary complex. Geophys Res Lett 38:L06310. View ArticleGoogle Scholar
  18. Huang WL, Otten GA (1998) Oil generation kinetics determined by DAC-FS/IR pyrolysis: technique development and preliminary results. Org Geochem 5–7:1119–1137. View ArticleGoogle Scholar
  19. Ishikawa T, Tanimizu M, Nagaishi K, Matsuoka J, Tadai O, Sakaguchi M, Hirono T, Mishima T, Tanikawa W, Lin W, Kikuta H, Soh W, Song S (2008) Coseismic fluid–rock interactions at high temperatures in the Chelungpu fault. Nat Geosci 1:679–683. View ArticleGoogle Scholar
  20. Ito K, Ujiie K, Kagi H (2017) Detection of increased heating and estimation of coseismic shear stress from Raman spectra of carbonaceous material in pseudotachylytes. Geophys Res Lett 44:1749–1757. Google Scholar
  21. Kameda J, Ujiie K, Yamaguchi A, Kimura G (2011) Smectite to chlorite conversion by frictional heating along a subduction thrust. Earth Planet Sci Lett 305:161–170. View ArticleGoogle Scholar
  22. Kaneki S, Hirono T, Mukoyoshi H, Sampei Y, Ikehara M (2016) Organochemical characteristics of carbonaceous materials as indicators of heat recorded on an ancient plate-subduction fault. Geochem Geophys Geosyst 17:2855–2868. View ArticleGoogle Scholar
  23. Kaneki S, Ichiba T, Hirono T (2018) Mechanochemical effect on maturation of carbonaceous material: implications for thermal maturity as a proxy for temperature in estimation of coseismic slip parameters. Geophys Res Lett 45:2248–2256. View ArticleGoogle Scholar
  24. Kitamura M, Mukoyoshi H, Fulton PM, Hirose T (2012) Coal maturation by frictional heat during rapid fault slip. Geophys Res Lett 39:L16302. View ArticleGoogle Scholar
  25. Kouketsu Y, Mizukami T, Mori H, Endo S, Aoya M, Hara H, Nakamura D, Wallis S (2014) A new approach to develop the Raman carbonaceous material geothermometer for low-grade metamorphism using peak width. Island Arc 23:33–50. View ArticleGoogle Scholar
  26. Kouketsu Y, Shimizu I, Wang Y, Yao L, Ma S, Shimamoto T (2017) Raman spectra of carbonaceous materials in a fault zone in the Longmenshan thrust belt, China; comparisons with those of sedimentary and metamorphic rocks. Tectonophysics 699:129–145. View ArticleGoogle Scholar
  27. Kuo LW, Felice FD, Spagnuolo E, Di Toro G, Song SR, Aretusini S, Li H, Suppe J, Si J, Wen CY (2017) Fault gouge graphitization as evidence of past seismic slip. Geology. Google Scholar
  28. Lewan MD (1997) Experiments on the role of water in petroleum formation. Geochem Cosmochem Acta 61:3691–3723. View ArticleGoogle Scholar
  29. Lievens C, Ci D, Bai Y, Ma L, Zhang R, Chen JY, Gai Q, Long Y, Guo X (2013) A study of slow pyrolysis of one low rank coal via pyrolysis–GC/MS. Fuel Process Technol 116:85–93. View ArticleGoogle Scholar
  30. Luque FJ, Ortega L, Barrenechea JF, Millward D, Beyssac O, Huizenga JM (2009) Deposition of highly crystalline graphite from moderate-temperature fluids. Geology 37:275–278. View ArticleGoogle Scholar
  31. Maekawa Y, Hirono T, Yabuta H, Mukoyoshi H, Kitamura M, Ikehara M, Tanikawa W, Ishikawa T (2014) Estimation of slip parameters associated with frictional heating during the 1999 Taiwan Chi–Chi earthquake by vitrinite reflectance geothermometry. Earth Planets Space 66:28. View ArticleGoogle Scholar
  32. Mishima T, Hirono T, Nakamura N, Tanikawa W, Soh W, Song S (2009) Changes to magnetic minerals caused by frictional heating during the 1999 Taiwan Chi–Chi earthquake. Earth Planets Space 61:797–801. View ArticleGoogle Scholar
  33. Mukoyoshi H, Sakaguchi A, Otsuki K, Hirono T, Soh W (2006) Co-seismic frictional melting along an out-of-sequence thrust in the Shimanto accretionary complex. Implications on the tsunamigenic potential of splay faults in modern subduction zones. Earth Planet Sci Lett 245:330–343. View ArticleGoogle Scholar
  34. Mukoyoshi H, Kaneki S, Hirono T (2018) Slip parameters on major thrusts at a convergent plate boundary: regional heterogeneity of potential slip distance at the shallow portion of the subducting plate. Earth Planets Space 70:36. View ArticleGoogle Scholar
  35. Nakamura Y, Oohashi K, Toyoshima T, Satish-Kumar M, Akai J (2015) Strain-induced amorphization of graphite in fault zones of the Hidaka metamorphic belt, Hokkaido, Japan. J Struct Geol 72:142–161. View ArticleGoogle Scholar
  36. O’Hara K (2004) Paleo-stress estimates on ancient seismogenic faults based on frictional heating of coal. Geophys Res Lett 31:L03601. Google Scholar
  37. Oohashi K, Han R, Hirose T, Shimamoto T, Omura K, Matsuda T (2014) Carbon-forming reactions under a reducing atmosphere during seismic fault slip. Geology 42:787–790. View ArticleGoogle Scholar
  38. Polissar PJ, Savage HM, Broadsky EE (2011) Extractable organic material in fault zones as a tool to investigate frictional stress. Earth Planet Sci Lett 311:439–447. View ArticleGoogle Scholar
  39. Rabinowitz HS, Polissar PJ, Savage HM (2017) Reaction kinetics of alkenone and n-alkane thermal alteration at seismic timescales. Geochem Geophys Geosyst 18:204–219. View ArticleGoogle Scholar
  40. Rowe C, Griffith WA (2015) Do faults preserve a record of seismic slip: a second opinion. J Struct Geol 78:1–26. View ArticleGoogle Scholar
  41. Sakaguchi A, Chester F, Curewitz D, Fabbri O, Goldsby D, Kimura G, Li CF, Masaki Y, Screaton EJ, Tsutsumi A, Ujiie K, Yamaguchi A (2011) Seismic slip propagation to the updip end of plate boundary subduction interface faults: vitrinite reflectance geothermometry on Integrated Ocean Drilling Program NanTroSEIZE cores. Geology 39:395–398. View ArticleGoogle Scholar
  42. Savage HM, Polissar PJ, Sheppard R, Rowe CD, Broadsky EE (2014) Biomarkers heat up during earthquakes: new evidence of seismic slip in the rock record. Geology 42:99–102. View ArticleGoogle Scholar
  43. Schenk HJ, Witte EG, Littke R, Schwochau K (1990) Structural modifications of vitrinite and alginite concentrates during pyrolytic maturation at different heating rates. A combined infrared, 13C NMR and microscopical study. Org Geochem 16:943–950. View ArticleGoogle Scholar
  44. Schito A, Romano C, Corrado S, Grigo D, Poe B (2017) Diagenetic thermal evolution of organic matter by Raman spectroscopy. Org Geochem 106:57–67. View ArticleGoogle Scholar
  45. Schleicher AM, Boles A, van der Pluijm BA (2015) Response of natural smectite to seismogenic heating and potential implications for the 2011 Tohoku earthquake in the Japan Trench. Geology 43:755–758. View ArticleGoogle Scholar
  46. Sheppard RE, Polissar PJ, Savage HM (2015) Organic thermal maturity as a proxy for frictional fault heating: experimental constraints on methylphenanthrene kinetics at earthquake timescales. Geochim Cosmochim Acta 151:103–116. View ArticleGoogle Scholar
  47. Sibson RH (1973) Interactions between temperature and pore-fluid pressure during earthquake faulting and a mechanism for partial or total stress relief. Nature 243:66–68. Google Scholar
  48. Spokas KA (2010) Review of the stability of biochar in soils: predictability of O: C molar ratios. Carbon Manag 1:289–303. View ArticleGoogle Scholar
  49. Stuart B (2004) Infrared spectrometry: fundamentals and applications. Wiley, Chichester, p 244View ArticleGoogle Scholar
  50. Tuinstra F, Koenig JL (1970) Raman spectrum of graphite. J Chem Phys 53:1126–1130. View ArticleGoogle Scholar
  51. Turian RM, Sung DJ, Hsu FL (1991) Thermal conductivity of granular coals, coal-water mixtures and multi-solid/liquid suspensions. Fuel 70:1157–1172. View ArticleGoogle Scholar


© The Author(s) 2018