- Express Letter
- Open Access
Changes in the b value in and around the focal areas of the M6.9 and M6.8 earthquakes off the coast of Miyagi prefecture, Japan, in 2021
Earth, Planets and Space volume 73, Article number: 176 (2021)
We investigated changes in the b value of the Gutenberg–Richter’s law in and around the focal areas of earthquakes on March 20 and on May 1, 2021, with magnitude (M) 6.9 and 6.8, respectively, which occurred off the Pacific coast of Miyagi prefecture, northeastern Japan. We showed that the b value in these focal areas had been noticeably small, especially within a few years before the occurrence of the M6.9 earthquake in its vicinity, indicating that differential stress had been high in the focal areas. The coseismic slip of the 2011 Tohoku earthquake seems to have stopped just short of the east side of the focus of the M6.9 earthquake. Furthermore, the afterslip of the 2011 Tohoku earthquake was relatively small in the focal areas of the M6.9 and M6.8 earthquakes, compared to the surrounding regions. In addition, the focus of the M6.9 earthquake was situated close to the border point where the interplate slip in the period from 2012 through 2021 has been considerably larger on the northern side than on the southern side. The high-stress state inferred by the b-value analysis is concordant with those characteristics of interplate slip events. We found that the M6.8 earthquake on May 1 occurred near an area where the b value remained small, even after the M6.9 quake. The ruptured areas by the two earthquakes now seem to almost coincide with the small-b-value region that had existed before their occurrence. The b value on the east side of the focal areas of the M6.9 and M6.8 earthquakes which corresponds to the eastern part of the source region of the 1978 off-Miyagi prefecture earthquake was consistently large, while the seismicity enhanced by the two earthquakes also shows a large b value, implying that stress in the region has not been very high.
An earthquake of magnitude (M) 6.9 occurred on March 20, 2021, at 18:09, on the Pacific coast of Miyagi prefecture, northeastern Japan, and successively, an M6.8 earthquake occurred on May 1, 2021, at 10:27, at about 50 km south of the M6.9 earthquake (Fig. 1a, b) (Earthquake Research Committee (ERC) 2021a, b, c). Both earthquakes were located on the periphery of the slip region of the 2011 M9.0 Tohoku earthquake (Fig. 1a), almost corresponding to the down-dip end of the interplate coupling zone between the overriding continental and the subducting Pacific plates (Igarashi et al. 2001). As can be seen in Fig. 1a, the foci of the two 2021 earthquakes were located in the area where the coseismic slip (orange contours) of the 2011 Tohoku earthquake was relatively large and the afterslip (black contours) during 7 months just after the earthquake occurrence was small compared to the surrounding region (Ozawa et al. 2012). Interestingly, it was reported that the focus of the M6.9 earthquake was situated at the border point where the interplate slip during the period from 2012 through 2021 inferred by the analysis of repeating earthquakes was large on the northern side and notably small on the southern side (Tohoku University 2021b).
When the M6.9 earthquake occurred on March 20, the ERC (2021a, b) pointed out that the focal area was located in the western part of the source region of the so-called off-Miyagi prefecture earthquake (Fig. 1b), an interplate earthquake that has occurred sequentially at intervals of about 38 years, the most recent one being the M7.4 earthquake in 1978 (green contours in Fig. 1a, b; Yamanaka and Kikuchi 2004). Note that the focal area of the M6.8 earthquake on May 1 was located at the west of the slip region of the M7.2 earthquake that occurred at off-Miyagi prefecture in 2005 (purple contours in Fig. 1a, b; Yaginuma et al. 2006). There was an overlap with the southeastern part of the source region of the 1978 off-Miyagi prefecture earthquake (Fig. 1b).
Here, we report the results of our analysis on spatio-temporal changes in the b value of the Gutenberg–Richter’s (GR) law (Gutenberg and Richter 1944) in and around the focal areas of the M6.9 and M6.8 earthquakes and in the source regions of the 1978 and 2005 off-Miyagi prefecture earthquakes, and discuss the implications of these results, noting the stress state on the plate interface in these regions.
We exploited the GR law, log10N = a − bM, where N is the number of events equal to or above M, and a and b are constants (Gutenberg and Richter 1944). Globally, on average, b ~ 1, but locally, b values show substantial spatial and temporal variation. In some cases, the proportion of earthquakes with large magnitudes is higher (b < 1), in others, the proportion of earthquakes with small magnitudes exceeds the average expectation (b > 1) (Figs. 2, 3, 4, 5).
To estimate b values consistently over space and time, we employed the Entire-Magnitude-Range (EMR) technique (Woessner and Wiemer 2005), which simultaneously calculates the completeness magnitude Mc, above which all events are considered to be detected by the referential seismic network. EMR applies the maximum-likelihood method represented by Eq. (6) of Utsu (1999) (e.g., Aki 1965; Utsu 1965) when computing the b value to events with magnitudes greater than Mc. We calculated the b values (Figs. 2, 3, 4, 5), provided that we found a minimum of 20 events with magnitudes greater than Mc for a given sample. We evaluated the uncertainty of the maximum-likelihood estimates of the b value, as described in Shi and Bolt (1982). The difference in b is not considered to be significant if the test proposed by Utsu (1992, 1999) is not passed. If logPb, the logarithm of the probability that the b values are not different, is equal to or smaller than − 1.3 (logPb ≤ − 1.3), then the difference in b is significant (Schorlemmer et al. 2004; Nanjo and Yoshida 2017). A fit of the GR law to observations for three circle areas is given in Fig. 3c, where the b value was estimated by the maximum-likelihood method (Aki 1965; Utsu 1965, 1999), rather than a coefficient of the GR law. The b value is smaller for the circle 1 (b = 0.4 ± 0.1) than for the circle 2 (b = 1.6 ± 0.1), taking an intermediate value for the circle 3 (b = 0.9 ± 0.2), indicating the significant difference in b among the three circle areas. This significance is further supported by the Utsu test (Utsu 1992, 1999; Schorlemmer et al. 2004; Nanjo and Yoshida 2017), revealing logPb1,3 (the logarithm of the probability that the b values for the circles 1 and 3 are not different) to be − 3.6, and logPb2,3 for the circles 2 and 3 to be − 4.5 (Fig. 3).
The b value is known to be sensitive to differential stress and its inverse correlation with differential stress has been evidenced by many laboratory and field studies (Mogi 1963; Scholz 1968, 2015; Lei 2003; Schorlemmer et al. 2005; Goebel et al. 2013). Investigation into space–temporal variation in b values to probe the stress state in the Earth's crust (Smith 1981; Schorlemmer et al. 2005; Narteau et al. 2009) has been applied to locate asperities (Hirose et al. 2002; Yabe 2003; Tormann et al. 2015; Nanjo and Yoshida 2018), and to estimate frictional properties (e.g., Sobiesiak et al. 2007; Ghosh et al. 2008) on the plate interface along subduction zones. Foreshocks have been known to show small b values (Suyehiro et al. 1964; Gulia and Wiemer 2019). Patches with small b values on active faults have been observed to coincide with locations of subsequent large earthquakes (Schorlemmer and Wiemer 2005; Nanjo et al. 2016, 2019; Nanjo 2020).
We used the Japan Meteorological Agency (JMA) earthquake catalog, which includes earthquakes since 1919 in and around Japan. Our analysis was based on earthquakes with M ≥ 0.5 during the period from January 1, 2012 through May 15, 2021, in a depth range of 0–100 km in the study region (Fig. 1b). We did not consider the period from immediately after the M9.0 Tohoku earthquake on March 11, 2011 to the end of 2011, avoiding the time period with large temporal variation in b. Most pre-shocks and aftershocks of the two M6.9 and M6.8 earthquakes in 2021 in the study region (Fig. 1b) occurred on and around the plate interface between the continental plate and the subducting Pacific plate (Fig. 3), so our primary approach was to develop maps about the b value and its cross sections.
A b-value analysis is critically dependent on a robust estimate of completeness of the processed earthquake data. In particular, underestimates in Mc lead to systematic underestimates in b values. We always paid attention to Mc when assessing Mc at each node and each time window (Additional file 1: Figures S1–S3). As discussed in other studies using the JMA catalog (Nanjo et al. 2010; Schorlemmer et al. 2018), Mc in offshore regions is expected to increase with distance from the coast, and Mc that had once increased during the period of an early aftershock sequence of the Tohoku earthquake, decreased afterward (Additional file 1: Figure S1). One of the reasons for this change in Mc was due to a change in the criterion for creating the JMA earthquake catalog in order to avoid the loss of integrity of work to determine hypocenters and the magnitudes of earthquakes (JMA 2012; Schorlemmer et al. 2018).
Figure 2a represents b maps in three periods: from January 1, 2012 through December 31, 2014, from January 1, 2015 through December 31, 2017, and from January 1, 2018 through March 20, 2021 before the occurrence of the M6.9 earthquake. The left panels of Fig. 3a, b are east–west cross-sectional views of b values, crossing the M6.9 and M6.8 hypocenters, respectively, based on seismicity (black circles in the right panels) from January 1, 2018 to immediately before the M6.9 earthquake (March 20, 2021, at 18:08). It is notable (Figs. 2 and 3) that the hypocenter of the M6.9 earthquake is located within an especially small-b-value structure (blue to purple) along the plate interface. The b value around the hypocenter of the M6.8 earthquake is also very small.
Note that the decrease in the b value in the area near the foci of the two 2021 earthquakes became conspicuous in later periods before the M6.9 earthquake (Fig. 2). In the first period, the local b value for the seismicity around the eventual M6.9 hypocenter was b = 0.8 ± 0.3 (light blue), nearly a global average (b ~ 1) (Fig. 3d). However, the b value in the intermediate period became 0.6 ± 0.2 (blue), and it decreased to a low value (0.4 ± 0.1) in the last period. As shown in Fig. 2b, the decrease in the b value around the focus of the 2021 M6.9 earthquakes in the last period relative to the first period was statistically significant (Utsu 1992, 1999; Schorlemmer et al. 2004; Nanjo and Yoshida 2017). The decrease in the b value in region A, a region surrounding focal areas of the 2021 M6.9 and M6.8 earthquakes, is also seen from Additional file 1: Figure S4 although the decrease in b is not clear in the focal area of the M6.8 earthquake as that in the focal area of the M6.9 earthquake (Additional file 1: Figures S5 and S6).
Incidentally, it might be worth noting that the b values in the middle panel of Fig. 2a are small in the focal area of the future M6.2 earthquake that occurred in 2020 (in the bottom panel of Fig. 2a).
Figure 4a shows a b map calculated for earthquakes that occurred during the period between the M6.9 and M6.8 earthquakes. It is notable that the b values in most parts of the focal regions of the two earthquakes, especially the southern part of the focal region of the M6.9 quake and the northern part of the focal region of the M6.8 quake in that period, were as small as those before the occurrence of the M6.9 earthquake, as is demonstrated by Fig. 4b, c. It might also be noteworthy that the b value for the seismicity induced in the eastern part of the source area of the 1978 off-Miyagi prefecture earthquake (green contours) seems to have increased after the M6.9 earthquake.
We also examined the temporal change in the b value in regions A and B shown in Fig. 5a during the period from January 1, 2018 through May 15, 2021. Similar to region A, region B corresponds to the eastern part of the source region of the 1978 off-Miyagi prefecture earthquake with M7.4, which includes the source area of the 2005 M7.2 earthquake that occurred at off-Miyagi prefecture. It is clear (Fig. 5b, c) that the b value in region A had been consistently small before the occurrence of the two earthquakes in 2021, and it is to be noted (Fig. 5c) that the small b-value state in region A continued after the occurrence of the M6.8 earthquake on May 1. This seems to indicate that a highly stressed state continued after the M6.8 earthquake in the area where the b value had been small before the M6.9 earthquake. Some possible interpretations of this result are discussed in the next section.
On the other hand, the b value in region B had been relatively large compared to the b value in region A throughout the whole period before the M6.9 earthquake, although region B showed a rather large range in b extending from 0.6 to 1.2 (Fig. 5). It is also worth noting that the large-b-value state in region B has been continuing not only after the occurrence of the M6.9 earthquake on March 20, but also after the M6.8 earthquake on May 1. We suppose this result suggests that the differential stress in the eastern part of the source region of the 1978 off-Miyagi prefecture earthquake has been relatively low throughout the entire study period.
By making maps and cross sections of the b value in the region around the foci of the March 20 and May 1, 2021, off-Miyagi prefecture earthquakes, we found that the b value in their focal areas had been considerably and consistently small and that the value became as low as 0.4–0.6 within a few years before their occurrence (Figs. 2 and 3). The distinct small b-value spot corresponded to the eventual M6.9 hypocenter (Figs. 2 and 3). This close match between the area of low and decreasing b values and the eventual M6.9 and M6.8 hypocenters supports the idea that the b value may be a stress meter for the Earth’s crust. Our finding also indicates that the stress before the M6.9 and M6.8 earthquakes had been high in the eventual focal areas, and the differential stress there had been heightened as time progressed. Here, it is to be noted that the coseismic slip of the 2011 Tohoku earthquake (orange contours in Fig. 1a) stopped just short of the east side of the focus of the M6.9 earthquake and the afterslip of the 2011 Tohoku earthquake in 7 months (black contours in Fig. 1a) had been relatively small in the focal areas of the two 2021 earthquakes, compared to the surrounding regions. Further, it is reported that the focus of the M6.9 earthquake was situated at the border point where the interplate slip during the period from 2012 through 2021 has been large on the northern side and notably smaller on the southern side (Tohoku University 2021b).
The appearance of the notably small-b-value spot might have been related to the characteristics of the interplate slip events. We believe our results present a clear additional example to supplement previous retrospective studies that showed a correlation between patches of small b values and sources of large earthquakes, e.g., at Izmit (Turkey), Parkfield and Ridgecrest (California), Tohoku and Kumamoto (Japan), and Iquique (Chile) (Wiemer and Wyss 2002; Schorlemmer and Wiemer 2005; Nanjo et al. 2012, 2016; Tormann et al. 2012, 2015; Schurr et al. 2014; Nanjo 2020).
It is notable that the b value for the events after the M6.9 earthquake on March 20, which occurred mainly near the southern end of the slip area had been as small as 0.5–0.6 (blue) (bottom panel of Fig. 2a and left panel of Fig. 3b). We should have focused our attention more on the observation that the events after the M6.9 earthquake showed a small b value and the rupture of the quake had not covered the whole small-b-value area that had existed before the quake, although it is not certain if we could have foreseen the occurrence of the M6.8 earthquake before May 1.
The finding that the b value that had appeared to be small before the M6.9 earthquake was still low after the M6.8 earthquake is somewhat an enigma (Fig. 5). This might mean that the two earthquakes had not fully unloaded the stress on the pre-existing asperity as interpreted for the Parkfield earthquake in 2004 (Tormann et al. 2012). However, we consider that such an interpretation cannot be applied to our case, because the rupture areas of the two earthquakes on March 20 and May 1 seem to cover almost entirely the small-b-value zone that had existed before their occurrence (bottom panel of Fig. 2a). One possible explanation may be that some patches with high stress had remained unruptured, and events after the M6.8 earthquake have been occurring there. The results of seismic source analysis of the M6.9 and M6.8 earthquakes (Tohoku University 2021a), which indicate a rather complex rupture process, seem to support this idea. Moreover, we would like to point out the occurrence of an M5.8 earthquake on April 18 at the far end of the rupture area of the earthquake on May 1 (Fig. 5a and Additional file 1: Figure S3c). The sequential occurrence of the M6.9, M5.8 and M6.8 earthquakes in the small-b-value zone that had been observed before these earthquakes indicates that there had existed at least three high-stress asperities. This also seems to imply that additional smaller patches might have remained unruptured.
ERC (2021a), after a meeting held on March 22, commented that it was necessary to pay attention to the occurrence of another large earthquake that might result in a similar or even stronger seismic intensity during the period of one week, especially in a few days. We suppose that, in the background of this caution, ERC (2021a) concerned about the occurrence of the so-called off-Miyagi prefecture earthquake that has been occurring sequentially at intervals of about 38 years, and whose probability of occurrence within the next 30 years was estimated to be about 60–70% as of January 1, 2021 (ERC 2021a,2021b). In addition, Nakata et al. (2016) based on numerical simulation, suggested that the time interval between the M ~ 9 earthquake and the subsequent earthquake off the coast of Miyagi prefecture would become shorter than the average recurrence interval during the later stage of the M ~ 9 earthquake cycle. As was pointed out in the Introduction, the two 2021 earthquakes occurred in the western part of the source region of the 1978 M7.4 off-Miyagi prefecture earthquake, and the focal area of the M6.8 earthquake is located west of the source region of the 2005 earthquake that occurred off the coast of Miyagi prefecture, fracturing the southern part of the source region of the 1978 earthquake (Fig. 1b). Therefore, it might not be unreasonable for ERC (2021a) to have been anxious about the possibility of the occurrence of a large earthquake on the east side of the focal areas of the two 2021 earthquakes.
Concerning this anxiety, we would like to note that the b value in the region had consistently been rather large before the two 2021 earthquakes and that the seismicity induced there by those earthquakes has been showing a large b value as well (Figs. 4 and 5). This indicates that stress in the region on the east side of the focal area of the two 2021 earthquakes had not been so high and the low-stress state has been continuing. Therefore, we conjecture that the probability of occurrence of a large earthquake in the adjacent region in the very near future may not be so large, although it is necessary to continue to watch for any signal that indicates change in local stress in the region.
This study revealed that the b value in and around the focal areas of the M6.9 and M6.8 earthquakes that occurred off the Pacific coast of Miyagi prefecture, northeastern Japan, on March 20 and May 1, 2021, respectively, had been considerably low before their occurrence. The b value in the vicinity of the M6.9 earthquake decreased to around 0.4 in the last few years. On the other hand, the b value on the east side of the focal areas that corresponds to the eastern part of the source region of the 1978 off-Miyagi prefecture earthquake had been relatively large during the whole period that was investigated. This result implies that the stress in the region had not been as high as the stress in the focal areas of the two earthquakes in 2021 and that the low-stress state there has been continuing.
Availability of data and materials
The JMA earthquake catalog was obtained from http://www.data.jma.go.jp/svd/eqev/data/bulletin/index_e.html. Coseismic slip of the 2021 M6.9 and M6.8 earthquakes determined by Keisuke Yoshida (Tohoku University 2021a) could be obtained from https://www.static.jishin.go.jp/resource/monthly/2021/2021_04.pdf. Copyright permission for the M6.9 and M6.8 slip-models was obtained from Keisuke Yoshida. An updated version of these models was given in a submitting paper (Yoshida K, Matsuzawa T, Uchida N (2021) The 2021 Mw7.0 Miyagi-Oki earthquake, northeastern Japan, nucleated from deep plate boundary: implications for the initiation of the M9 earthquake cycle. Submitted to Journal of Geophysical Research—Solid Earth). This preprint is available at https://doi.org/10.1002/essoar.10507585.1 (Accessed on August 31, 2021). Coseismic and postseismic slips of the 2011 Tohoku earthquake were obtained from Fig. 12 of Ozawa et al. (2012). Coseismic slips of the 1978 M7.4 off-Miyagi prefecture earthquake and the 2005 M7.2 earthquake that occurred at off-Miyagi prefecture were obtained from Yamanaka and Kikuchi (2004) and Yaginuma et al. (2006), respectively. The upper surface of the Pacific plate (Nakajima and Hasegawa 2006) was obtained from https://www.mri-jma.go.jp/Dep/sei/fhirose/plate/en.index.html. Focal mechanism catalog of F-net (Okada et al. 2004) was obtained from https://www.fnet.bosai.go.jp/top.php?LANG=en.
Earthquake Research Committee
Full Range Seismograph Network of Japan
- GR law:
Japan Meteorological Agency
- M :
- M c :
Magnitude of completeness (or completeness magnitude)
National Research Institute for Earth Science and Disaster Resilience
Aki K (1965) Maximum likelihood estimates of b in the formula logN=a-bM and its confidence limits. Bull Earthquake Res Inst Univ Tokyo 43(2):237–239
Earthquake Research Committee (2021a) Evaluation of the March 20, 2021, earthquake that occurred at off-Miyagi prefecture, released on March 22, 2021. (In Japanese). https://www.static.jishin.go.jp/resource/monthly/2021/20210320_miyagi_1.pdf. Accessed 31 Aug 2021
Earthquake Research Committee (2021b) Evaluation of the March 20, 2021, earthquake that occurred at off-Miyagi prefecture, released on April 9, 2021. (In Japanese). https://www.static.jishin.go.jp/resource/monthly/2021/20210320_miyagi_2.pdf. Accessed 31 Aug 2021
Earthquake Research Committee (2021c) Evaluation of seismicity in April 2021. (In Japanese). https://www.static.jishin.go.jp/resource/monthly/2021/2021_04.pdf. Accessed 31 Aug 2021
Ghosh A, Newman AV, Thomas AM, Farmer GT (2008) Interface locking along the subduction megathrust from b-value mapping near Nicoya Peninsula, Costa Rica. Geophys Res Lett 35:L01301. https://doi.org/10.1029/2007GL031617
Goebel THW, Schorlemmer D, Becker TW, Dresen G, Sammis CG (2013) Acoustic emissions document stress changes over many seismic cycles in stick-slip experiments. Geophys Res Lett 40:2049–2054. https://doi.org/10.1002/grl.50507
Gulia L, Wiemer S (2019) Real-time discrimination of earthquake foreshocks and aftershocks. Nature 574:193–199. https://doi.org/10.1038/s41586-019-1606-4
Gutenberg B, Richter CF (1944) Frequency of earthquakes in California. Bull Seismol Soc Am 34(4):185–188. https://doi.org/10.1785/BSSA0340040185
Hirose F, Nakamura A, Hasegawa A (2002) b-value variation associated with the rupture of asperities-Spatial and temporal distributions of b-value east off NE Japan (in Japanese). J Seismol Soc Jpn 55(3):249–260. https://doi.org/10.4294/zisin1948.55.3_249
Igarashi T, Matsuzawa T, Umino N, Hasegawa A (2001) Spatial distribution of focal mechanisms for interplate and intraplate earthquakes associated with the subducting Pacific plate beneath the northeastern Japan arc: a triple-planed deep seismic zone. J Geophys Res 106(B2):2177–2191. https://doi.org/10.1029/2000JB900386
Japan Meteorological Agency (2012) The criterion of hypocenter determination process and the earthquake detection level after the 2011 off the Pacific coast of Tohoku Earthquake (In Japanese). Report of the Coordinating Committee for Earthquake Prediction, Japan 87: 8–13. https://cais.gsi.go.jp/YOCHIREN/report/kaihou87/01_03.pdf. Accessed 31 Aug 2021.
Lei X (2003) How do asperities fracture? An experimental study of unbroken asperities. Earth Planet Sci Lett 213(3–4):347–359. https://doi.org/10.1016/S0012-821X(03)00328-5
Mogi K (1963) The fracture of a semi-infinite body caused by an inner stress origin and its relation to the earthquake phenomena (Second Paper): The case of the materials having some heterogeneous structures. Bull Earthquake Res Inst Univ Tokyo 41(3):595–614
Nakajima J, Hasegawa A (2006) Anomalous low-velocity zone and linear alignment of seismicity along it in the subducted Pacific slab beneath Kanto, Japan: Reactivation of subducted fracture zone? Geophys Res Lett 33:L16309. https://doi.org/10.1029/2006GL026773
Nakata R, Hori T, Hyodo M, Ariyoshi K (2016) Possible scenarios for occurrence of M ~ 7 interplate earthquakes prior to and following the 2011 Tohoku-Oki earthquake based on numerical simulation. Sci Rep 6:25704. https://doi.org/10.1038/srep25704
Nanjo KZ (2020) Were changes in stress state responsible for the 2019 Ridgecrest, California, earthquakes? Nat Commun 11:3082. https://doi.org/10.1038/s41467-020-16867-5
Nanjo KZ, Yoshida A (2017) Anomalous decrease in relatively large shocks and increase in the p and b values preceding the April 16, 2016, M7.3 earthquake in Kumamoto, Japan. Earth Planets Space 69:13. https://doi.org/10.1186/s40623-017-0598-2
Nanjo KZ, Yoshida A (2018) A b map implying the first eastern rupture of the Nankai Trough earthquakes. Nat Commun 9:1117. https://doi.org/10.1038/s41467-018-03514-3
Nanjo KZ, Ishibe T, Tsuruoka H, Schorlemmer D, Ishigaki Y, Hirata N (2010) Analysis of the completeness magnitude and seismic network coverage of Japan. Bull Seismol Soc Am 100(6):3261–3268. https://doi.org/10.1785/0120100077
Nanjo KZ, Hirata N, Obara K, Kasahara K (2012) Decade-scale decrease in b value prior to the M9-class 2011 Tohoku and 2004 Sumatra quakes. Geophys Res Lett 39:L20304. https://doi.org/10.1029/2012GL052997
Nanjo KZ, Izutsu J, Orihara Y et al (2016) Seismicity prior to the 2016 Kumamoto earthquakes. Earth Planets Space 68:187. https://doi.org/10.1186/s40623-016-0558-2
Nanjo KZ, Izutsu J, Orihara Y, Kamogawa M, Nagao Y (2019) Changes in seismicity pattern due to the 2016 Kumamoto earthquakes identify a highly stressed area on the Hinagu fault zone. Geophys Res Lett 46(16):9489–9496. https://doi.org/10.1029/2019GL083463
Narteau C, Byrdina S, Shebalin P, Schorlemmer D (2009) Common dependence on stress for the two fundamental laws of statistical seismology. Nature 462:642–645. https://doi.org/10.1038/nature08553
Okada Y, Kasahara K, Hori S, Obara K, Sekiguchi S, Fujiwara H, Yamamoto A (2004) Recent progress of seismic observation networks in Japan-Hi-net, F-net K-NET and KiK-net. Earth Planets Space 56(8):xv–xxviii. https://doi.org/10.1186/BF03353076
Ozawa S, Nishimura T, Munekane H, Suito H, Kobayashi T, Tobita M, Imakiire T (2012) Preceding, coseismic, and postseismic slips of the 2011 Tohoku earthquake, Japan. J Geophys Res 117(B7):B07404. https://doi.org/10.1029/2011JB009120
Scholz CH (1968) The frequency-magnitude relation of microfracturing in rock and its relation to earthquakes. Bull Seismol Soc Am 58(1):399–415
Scholz CH (2015) On the stress dependence of the earthquake b value. Geophys Res Lett 42(5):1399–1402. https://doi.org/10.1002/2014GL062863
Schorlemmer D, Wiemer S (2005) Microseismicity data forecast rupture area. Nature 434:1086. https://doi.org/10.1038/4341086a
Schorlemmer D, Wiemer S, Wyss M (2004) Earthquake statistics at Parkfield: 1. Stationarity of b values. J Geophys Res 109:B12307. https://doi.org/10.1029/2004JB003234
Schorlemmer D, Wiemer S, Wyss M (2005) Variations in earthquake-size distribution across different stress regimes. Nature 437:539–542. https://doi.org/10.1038/nature04094
Schorlemmer D, Hirata N, Ishigaki Y, Doi K, Nanjo KZ, Tsuruoka H, Beutin T, Euchner F (2018) Earthquake detection probabilities in Japan. Bull Seismol Soc Am 108(2):702–717. https://doi.org/10.1785/0120170110
Schurr B, Asch G, Hainzl S et al (2014) Gradual unlocking of plate boundary controlled initiation of the 2014 Iquique earthquake. Nature 512:299–302. https://doi.org/10.1038/nature13681
Shi Y, Bolt BA (1982) The standard error of the magnitude-frequency b value. Bull Seismol Soc Am 72(5):1677–1687. https://doi.org/10.1785/BSSA0720051677
Smith WD (1981) The b-value as an earthquake precursor. Nature 289:136–139. https://doi.org/10.1038/289136a0
Sobiesiak M, Meyer U, Schmidt S, Götze H-J, Krawczyk CM (2007) Asperity generating upper crustal sources revealed by b value and isostatic residual anomaly grids in the area of Antofagasta, Chile. J Geophys Res 112:B12308. https://doi.org/10.1029/2006JB004796
Suyehiro S, Asada T, Ohtake M (1964) Foreshocks and aftershocks accompanying a perceptible earthquake in central Japan—On the peculiar nature of foreshocks—Papers. Meteorol Geophys 15:71–88. https://doi.org/10.2467/mripapers1950.15.1_71
Tohoku University (2021a) Coseismic slip distribution estimated from waveform inversion of the May 1, 2021, off Miyagi prefecture earthquake. In: ERC (ed) Evaluation of seismicity in April 2021, pp 18. (In Japanese). https://www.static.jishin.go.jp/resource/monthly/2021/2021_04.pdf. Accessed 31 Aug 2021
Tohoku University (2021b) Space-temporal change in the slip rate. In: Report of the 231st Coordinating Committee for Earthquake Prediction, Japan, May 22–28, 2021. (In Japanese). https://cais.gsi.go.jp/YOCHIREN/activity/231/image231/030.pdf. Accessed 31 Aug 2021
Tormann T, Wiemer S, Hardebeck JL (2012) Earthquake recurrence models fail when earthquakes fail to reset the stress field. Geophys Res Lett 39(18):L18310. https://doi.org/10.1029/2012GL052913
Tormann T, Enescu B, Woessner J, Wiemer S (2015) Randomness of megathrust earthquakes implied by rapid stress recovery after the Japan earthquake. Nat Geosci 8:152–158. https://doi.org/10.1038/ngeo2343
Utsu T (1965) A method for determining the value of b in a formula logn=a-bM showing the magnitude-frequency relation for earthquakes. Geophys Bull Hokkaido Univ 13:99–103. (in Japanese). https://doi.org/10.14943/gbhu.13.99
Utsu T (1992) On seismicity. In: Report of the joint research institute for statistical mathematics, Inst Stat Math Tokyo. vol 34, pp 139–157.
Utsu T (1999) Representation and analysis of the earthquake size distribution: a historical review and some approaches. Pure Appl Geophys 155(2):509–535. https://doi.org/10.1007/s000240050276
Wessel P, Smith WHF, Scharroo R, Luis J, Wobbe F (2013) Generic mapping tools: improved version released. EOS Trans AGU 94:409–410. https://doi.org/10.1002/2013EO450001
Wiemer S (2001) A software package to analyze seismicity: ZMAP. Seismol Res Lett 72(3):373–382. https://doi.org/10.1785/gssrl.72.3.373
Wiemer S, Wyss M (2002) Mapping spatial variability of the frequency-magnitude distribution of earthquakes. Adv Geophys 45:259–302. https://doi.org/10.1016/S0065-2687(02)80007-3
Woessner J, Wiemer S (2005) Assessing the quality of earthquake catalogues: estimating the magnitude of completeness and its uncertainty. Bull Seismol Soc Am 95(2):684–698. https://doi.org/10.1785/0120040007
Yabe Y (2003) Frictional property of plate interface east off NE Japan inferred from spatial variation in b-value. Bull Earthquake Res Inst Univ Tokyo 78(1):107–111
Yaginuma T, Okada T, Yagi Y, Matsuzawa T, Umino N, Hasegawa A (2006) Coseismic slip distribution of the 2005 off Miyagi earthquake (M7.2) estimated by inversion of teleseismic and regional seismograms. Earth Planets Space 58:1549–1554. https://doi.org/10.1186/BF03352659
Yamanaka Y, Kikuchi M (2004) Asperity map along the subduction zone in northeastern Japan inferred from regional seismic data. J Geophys Res 109(B7):B07307. https://doi.org/10.1029/2003JB002683
We would like to express our sincere thanks to the Editors (A. Kato and N. Uchida) and two anonymous reviewers for their very useful comments and suggestions that have improved the manuscript greatly. The authors thank the JMA for the earthquake catalog, T. Nagao for help with acquisition of this catalog, and K. Yoshida for copyright permission to use the M6.9 and M6.8 slip-models (Tohoku University 2021a). The seismicity analysis software package ZMAP (Wiemer 2001), used for Figs. 2, 3, 4, 5 and Additional file 1: Figures S1–S6, was obtained from http://www.seismo.ethz.ch/en/research-and-teaching/products-software/software/ZMAP. The Generic Mapping Tools (Wessel et al. 2013), used for Figures 1, 2, 4, and 5, and Additional file 1: Figures S1 and S3–6, are an open-source collection (https://www.generic-mapping-tools.org).
This study was partially supported by JSPS KAKENHI Grant Number JP 20K05050, the Tokio Marine Kagami Memorial Foundation, the Chubu Electric Power’s research based on selected proposals, and the Ministry of Education, Culture, Sports, Science and Technology (MEXT) of Japan, under the Second Earthquake and Volcano Hazards Observation and Research Program (Earthquake and Volcano Hazard Reduction Research) and under the STAR-E (Seismology TowArd Research innovation with data of Earthquake) Program Grant Number JPJ010217.
Ethics approval and consent to participate
Consent for publication
The authors declare that they have no competing interests.
Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Map of Mc. (a-c) Same as Fig. 2a for Mc. (d) Same as Fig. 4a for Mc. Figure S2. Cross-sectional views of Mc. (a,b) Same as left panels of Fig. 3a,b for Mc. Figure S3. Same as Fig. 5 for Mc. The uncertainty in the single Mc value estimates is according to Woessner and Wiemer (2005). Figure S4. Same as Fig. 5 for the period from 2012. (b) Region A. (c) Region B. Figure S5. Time-dependent b values for the rupture areas of the 2021 M6.9 and M6.8 earthquakes. (a) Map showing polygon regions surrounding slip contours of the M6.9 (red) and M6.8 (blue) earthquakes. Stars indicates the epicenters of the M6.9 March 20 earthquake, the M5.8 April 18 earthquake, and the M6.8 May 1 earthquake. Other symbols are as in Fig. 1. (b) Plot of b values as a function of time for the polygon regions surrounding slip contours of the M6.9 (red) and M6.8 (blue) earthquakes. In constructing this figure, we applied the same plotting procedure as for Fig. 5, except for a longer time period (from 2012 to the present) and smaller regions (the polygon regions). Figure S6. Same as Fig. S5 for regions of slip contours of 0.4 m (outer contours) of the M6.9 (red) and M6.8 (blue) earthquakes.
It includes numerical data that list the longitude and latitude consisting of slip contours of the M6.9 earthquake.
It includes numerical data that list the longitude and latitude consisting of slip contours of the M6.8 earthquake.
About this article
Cite this article
Nanjo, K.Z., Yoshida, A. Changes in the b value in and around the focal areas of the M6.9 and M6.8 earthquakes off the coast of Miyagi prefecture, Japan, in 2021. Earth Planets Space 73, 176 (2021). https://doi.org/10.1186/s40623-021-01511-3
- Statistical analysis
- Earthquake dynamics
- Seismicity and tectonics
- Earthquake interaction
- and prediction
- Computational seismology
- Spatial analysis
- Time series analysis
- Subduction zone processes