Open Access

A 3-D electrical resistivity model beneath the focal zone of the 2008 Iwate-Miyagi Nairiku earthquake (M 7.2)

  • Hiroshi Ichihara1, 2Email author,
  • Shin'ya Sakanaka3,
  • Masaaki Mishina4,
  • Makoto Uyeshima2,
  • Tadashi Nishitani3,
  • Yasuo Ogawa5,
  • Yusuke Yamaya6,
  • Toru Mogi7,
  • Kazuhiro Amita3 and
  • Takuya Miura3, 8
Earth, Planets and Space201466:50

Received: 11 December 2013

Accepted: 26 May 2014

Published: 10 June 2014


The 2008 Iwate-Miyagi Nairiku earthquake (M 7.2) was a shallow inland earthquake that occurred in the volcanic front of the northeastern Japan arc. To understand why the earthquake occurred beneath an active volcanic area, in which ductile crust generally impedes fault rupture, we conducted magnetotelluric surveys at 14 stations around the epicentral area 2 months after the earthquake. Based on 56 sets of magnetotelluric impedances measured by the present and previous surveys, we estimated the three-dimensional (3-D) electrical resistivity distribution. The inverted 3-D resistivity model showed a shallow conductive zone beneath the Kitakami Lowland and a few conductive patches beneath active volcanic areas. The shallow conductive zone is interpreted as Tertiary sedimentary rocks. The deeper conductive patches probably relate to volcanic activities and possibly indicate high-temperature anomalies. Aftershocks were distributed mainly in the resistive zone, interpreted as a brittle zone, and not in these conductive areas, interpreted as ductile zones. The size of the brittle zone seems large enough for a fault rupture area capable of generating an M 7-class earthquake, despite the areas distributed among the ductile zones. This interpretation implies that 3-D elastic heterogeneity, due to regional geology and volcanic activities, controls the size of the fault rupture zone. Additionally, the elastic heterogeneities could result in local stress concentration around the earthquake area and cause faulting.


Magnetotelluric Iwate-Miyagi earthquake 3-D resistivity Inland earthquake



The 2008 Iwate-Miyagi Nairiku earthquake (M 7.2) was an inland earthquake that occurred in the vicinity of the volcanic front of the northeastern Japan arc on 14 July 2008. The focal mechanism of the earthquake was a reverse type, which is consistent with the crustal deformation displaying east–west contraction around the study area (Miura et al. 2002, 2004). Aftershocks of the earthquake were distributed within an area of 50 × 15 km and showed a complex distribution (Figure 1) (Okada et al. 2012). A curious feature of the earthquake was that volcanic areas (Mt. Kurikoma, Mt. Yakeishi, and Onikobe Caldera) surrounded the earthquake area. In general, ductile areas caused by high temperature and partial melting are distributed beneath volcanic regions. Because these ductile areas impede the propagation of fault ruptures, it would seem difficult for large earthquakes to occur in volcanic regions. To address this question and better understand the relationships between inland earthquakes and volcanic activity, detailed structural investigations are required.
Figure 1

Study locations. The red star and red triangles denote the epicenter of the 2008 Iwate-Miyagi Nairiku earthquake (M 7.2) and active volcanoes, respectively. (a) The yellow circle denotes the remote reference site (Sawauchi station). The cross-hatched area indicates the Kitakami Lowland. (b) Yellow diamonds and triangles denote MT stations in this and a previous study (Mishina 2009), respectively. Small red dots denote aftershocks of the 2008 earthquake (Okada et al. 2012).

The magnetotelluric (MT) method reveals the distribution of electrical resistivity and has been used to clarify the geology, high-temperature anomalies, and fluid distribution around earthquake zones (e.g., Mitsuhata et al. 2001; Ogawa et al. 2001; Sarma et al. 2004; Unsworth and Bedrosian, 2004; Ichihara et al. 2008, 2009, 2011; Wannamaker et al. 2009; Yoshimura et al. 2009). Mishina (2009) conducted MT surveys along three survey lines across the northern edge, central part, and southern edge of the aftershock area (Figure 1) and estimated resistivity distributions based on two-dimensional (2-D) inversions. The models showed low-resistivity anomalies around the earthquake area that imply crustal fluid flows. They also showed significant differences among the resistivity profiles, which indicate strong three-dimensionality. However, 2-D inversion of a strong three-dimensional (3-D) resistivity structure often results in inaccurate models (e.g., Siripunvaraporn et al. 2005b). Additionally, MT data were not measured around the epicenter of the main shock. In this study, we conducted wide-band MT measurements around the epicentral area and updated the resistivity models based on a 3-D inversion. Then, we interpreted the geological and thermal heterogeneity based on the estimated resistivity model and discussed the relationship between the earthquake and these heterogeneities.

Magnetotelluric measurements and impedances

Wide-band MT surveys were conducted at 14 sites along a profile passing through the epicenter of the earthquake in August 2008 (Figure 1). We recorded two horizontal components of electric field and three components of magnetic field using MTU2000 systems (Phoenix Geophysics, Ltd., Toronto, Canada). The electric and magnetic fields were measured using Pb-PbCl2 electrodes and induction coils, respectively. The recorded time series were converted into frequency-domain MT impedance tensors between 320 and 0.00034 Hz by using the SSMT200 system (Phoenix Geophysics, Ltd.). The remote reference technique (Gamble et al. 1979) was applied in the estimation of MT impedances using horizontal magnetic field data from Sawauchi station (Figure 1), which yielded high-quality MT responses.

We then evaluated the dimensionality of the resistivity distribution based on MT impedances and geomagnetic transfer functions at 56 sites: 14 sites evaluated by this study, 41 sites by Mishina (2009), and 1 site by the Geographical Survey Institute. Figure 2 shows the phase tensor ellipses (Caldwell et al. 2004) and Parkinson's induction vectors (Parkinson 1962). The azimuths of Φmax (α - β) in the phase-tensor ellipses were directed dominantly toward 115° to 295° in the long period (227 s in Figure 2). This azimuth is perpendicular to the strike azimuth of the NE Japan arc. On the other hand, no obvious trend was found from the phase tensor in the shorter period or the induction vectors in all periods (Figure 2). Additionally, large |β| values (>10°) were recognized in more than half of the phase tensors in the long period. These indicate that the resistivity distribution was highly three-dimensional.
Figure 2

Phase tensor ellipses and induction vectors. Large ellipses denote observed phase tensor ellipses, whereas small ones in the background denote synthetic ellipses at respective virtual sites, which were calculated from the 3-D resistivity model. The color of the ellipse denotes Φmin, Φmin, and β for (a), (b), and (c), respectively. Purple arrows in (c) denote the observed real part of Parkinson's induction vectors (Parkinson 1962). Note that we exclude observed values showing large error exceeding 5°, 5°, 2°, and 0.05 for Φmin, Φmax, β, and induction vector, respectively.

Three-dimensional inversion

The 3-D resistivity distribution was estimated based on the 56 MT impedances via a 3-D inversion code. We adopted the WSINV3D code (Siripunvaraporn et al. 2005a), which is based on a data-space variant of the Occam approach, for the inversion. Twelve periods of MT impedances between 0.44 and 990 s were used as input for the inversion. Error floors of 10% and 20% were applied for off-diagonal and diagonal components, respectively. The 3-D resistivity model covered a 4,000 (x-axis) × 4,000 (y-axis) × 1,240 km (vertical) region discretized into 54 × 65 × 31 layers (without air layers). The length and width of the blocks within the survey area were 2 km, but these widened outside the study area. The initial inversion model consisted of a 300 Ω m homogeneous half-space model, except for the seawater area. The model blocks in the seawater area were fixed to 0.3 Ω m. The same model used for the initial model was adapted as a prior model. We iterated the inversion procedure 10 times and obtained a minimum RMS misfit model in the sixth iteration (RMS misfit 2.54). Then, we adopted the sixth iteration model as the initial and prior model and reran the inversion procedures 10 times. Finally, a minimum RMS misfit model was obtained in the second iteration of the second procedure (RMS misfit 1.53). The final inverted resistivity model mostly explained all components of the measured impedances (Figure 3). The model showed distinct conductors around the aftershock area (Figures 4 and 5): a shallow conductor (1 to 10 Ω m) beneath the Kitakami Lowland (C-1); conductors beneath the volcanic areas of Mt. Kurikoma (C-2), Onikobe Caldera (C-3a), and Mukaimachi Caldera (C-3b); and conductors distributed beneath the C-1 conductor (C-4 and C-5). On the other hand, high resistivity (100 to 10,000 Ω m) was estimated in the mainshock and aftershock areas.
Figure 3

Apparent resistivities and impedance phases. Dots with error bars and solid lines are based on measured impedances and calculated impedances of the inverted model. The dashed, dash-dotted, and dotted lines denote the calculated impedances of the sensitivity tests (see text for details).

Figure 4

Horizontal cross sections of the inverted resistivity model. The pink diamonds denote MT stations. The red star and red dots denote the epicenters of the mainshock and its aftershocks, respectively. The dashed lines indicate replaced areas in the sensitivity tests. The thin lines denoted as ‘Y,’ ‘I,’ ‘K,’ and ‘N’ indicate the locations of the cross sections in Figure 5.

Figure 5

Vertical cross sections of the inverted resistivity model. The red arrows indicate the area of the Kitakami Lowland. The other symbols are the same as in Figure 4.

High Φmax and Φmin (>45°) in short-period data (<1 s) in the Kitakami Lowland required the C-1 conductor (Figure 2). Induction vectors around the middle period (1 to 30 s) directed to the Kitakami Lowland supported the C-1 conductor. The C-2, C-3a, C-4, and C-5 conductors were verified based on the following sensitivity tests. If the area enclosed by the black dashed line around C-2 in Figures 4 and 5 was given a uniform resistivity of 300 Ω m, the RMS misfit for all the MT sites was increased to 1.895 from 1.530 in the inverted model. In this sensitivity test, the calculated phases in the YX component were decreased more than 10° at site K180 in the periods between 0.885 and 7.09 s compared with the measured impedances and the response of the inverted model (Figure 3). Similarly, the sounding curves in the MT sites near the C-3a, C-4, and C-5 conductors and the total RMS misfits were significantly changed when these conductors were replaced with 300 Ω m (Table 1 and Figure 3). The resistive zone around the earthquake area (R-1) was also verified based on the following sensitivity test. If the area enclosed by white dashed line in Figures 4 and 5 was given with 30 Ω m, the RMS misfit was increased to 2.906 and the calculated MT impedances were significantly changed in the short-middle period band (<100 s) (Figure 3).
Table 1

The RMS misfits of the sensitivity test models (see text for details)


Inverted model

3 Ω m

10 Ω m

30 Ω m

100 Ω m

300 Ω m





























The resistivities in the first row indicate filled resistivities in the tests. RMS misfits indicating significant differences compared with the inverted model are italicized. The significances are based on the F test at the 95% confidence level. All models have 5,375 degrees of freedom.

We next constrained the reliable resistivity ranges of the C-2, C-3a, C-4, and C-5 conductors based on the following additional sensitivity tests (Toh et al. 2006). In these tests, we replaced the conductors in the inverted model with 100, 30, and 10 Ω m. The replaced areas are enclosed by dashed lines in Figures 4 and 5, except for the blocks that showed lower resistivity than the replacing resistivities. The RMS misfits of these models are shown in Table 1. To examine whether the filled test models were significantly different from the original inverted models, we adopted the F test. Based on the F test with a 95% confidence level, C-2, C-3a, C-4, and C-5 with resistivities higher than 30, 30, 30, and 100 Ω m, respectively, were significantly worse compared with the original inverted model, which indicated that the resistivity of the conductors should be lower than these resistivities.


Although C-1, C-2, C-3b, C-4, and C-5 were also found in the previous study based on the 2-D inversion method (Mishina 2009), their shapes and distribution depths are different in the present model. The C-2 and C-3b conductors are in shallower areas in the 3-D model than in the 2-D models. This inconsistency is probably due to inaccuracy in the 2-D inversion, because large |β| values (>10°) above C-2 and C-3b (Figure 2) indicate a strong 3-D effect in the MT impedances. Additionally, a conductor beneath Mt. Yakeishi in the 2-D model does not occur in the 3-D model. The likely reason for this difference in the models is that the 2-D inversion may have detected C-2, which is distributed alongside but not below the 2-D survey line (Figure 4), because 2-D inversion often shows conductors distributed off the profile (e.g., Siripunvaraporn et al. 2005b).

The C-1 conductor reflects Tertiary sedimentary rocks because these rocks show low resistivity (1 to 10 Ω m) in the NE Japan area (Takakura 1995; Ichihara et al. 2011) and are distributed from the surface to a depth of 3,000 m (maximum) beneath the Kitakami Lowland, according to geological and seismic surveys (e.g., Kato et al. 2006). However, the C-1 conductor is not shown in blank areas of the MT stations (between lines Y and I and east of line N), although seismic surveys found thick sediment in these areas (Kato et al. 2006). In order to assess the impact of the surface conductive sediment in the blank areas to the present MT data, we filled these areas (purple dashed line in Figure 4, depth 0.5 to 3.0 km) in the inverted model with conductor (5 Ω m) and calculated MT impedances (‘test C-1’ in Figure 3). The calculated impedances are slightly changed from these of the inverted model except for the long-period impedances in the eastern part of C-1 area where deep conductors such as C-4 and C-5 also affect the long-period MT responses as we discuss later. This indicates that the present MT data are hard to detect C-1 in the blank areas, and thus, conductors are possibly distributed. On the other hand, the resistive zone including R-1 beneath C-1 and the aftershock area is reliable regardless of the shape of C-1 conductor because it slightly affects the MT impedances above the R-1 while the MT responses are significantly changed when R-1 is covered with 30 Ω m (sites Y170 and I820 in Figure 3). The R-1 are interpreted as granites because these rocks are distributed beneath the Tertiary sedimentary rocks and are a basement rock of the NE Japan arc (e.g., Sato 1994).

The C-2 conductor is distributed beneath Mt. Kurikoma, which has displayed Quaternary volcanic activity (Fujinawa et al. 2001). Okada et al. (2010) indicated a low-velocity (Vs) anomaly in this area that was interpreted as partial melting. They inferred that the melt originated from upwelling flow in the mantle wedge (e.g., Hasegawa et al. 2005). Thus, C-2 can be interpreted as high-temperature or partial melt zones related to volcanic activities. Assuming that C-2 consists of a silicic composition and contains 2.5 to 3.0 wt% or 0 wt% H2O, the temperature of C-2 (<30 Ω m) would be 500°C or 600°C, respectively, based on Gaillard (2004) (Figure 6). Similarly, the temperature of C-3a (<30 Ω m), which is distributed beneath the Onikobe Caldera, should be more than 500°C. In contrast, the temperature in the non-volcanic area of the volcanic front area at a depth of 8 km should be 210°C, assuming a heat flow of 80 mW/m2 (based on Tanaka and Ishikawa (2002) and Tanaka et al. (2004)). Therefore, the temperature in the areas of the C-2 and C-3a conductors should be 200°C higher than that of the surrounding area, assuming that high temperature causes the conductive anomalies. The actual temperature in the areas of the C-2 and C-3a conductors, however, should be higher than these estimates for the following reasons: (1) andesite, which requires a higher temperature to explain the same resistivity, as compared to silicic material (e.g., Gaillard and Marziano 2005), is distributed in the Kurikoma volcano (Fujinawa et al. 2001) and (2) the actual resistivity in the conductive areas should, in part, be lower than 30 Ω m because the inverted model shows a value of 1 Ω m in the centers of the C-2 and C-3a conductors and the inversion adopted a smoothness constraint. Partial melt or a large amount of aqueous fluid may be required to explain such a low resistivity. For better constraint, additional surveys are required, especially for the C-3a conductor, which does not include an MT station.
Figure 6

Resistivity of obsidians based on Figure seven in Gaillard (2004). Diamonds denote laboratory measurements of resistivity for hydrous obsidians. Red and blue lines are estimated resistivity based on the Arrhenius law. The resistivity of dry obsidian (black line) is calculated from the results of different pressure conditions. The green dashed line denotes the resistivity range of the C-2 and C-3a conductors.

The C-4 conductor is possibly required to explain out-of-quadrant phases in the YX component at sites Y200, Y210, and Y220 because the anomalous large phases are not explained when the C-4 conductor is filled with 300 Ω m (Figure 3). Similarly, out-of-quadrant phases observed at site I823 are not explained when C-5 is filled with 300 Ω m (Figure 3). On the other hand, strong channeling of telluric current due to the shallow conductor beneath the Kitakami Lowland (C-1) is also a candidate for the anomalous large phases because a shallow conductor complex sometimes induces out-of-quadrant phases (e.g., Ichihara and Mogi 2009; Ichihara et al. 2013). Indeed, the above hypothesis model that the conductor is inserted in the blank areas of the MT sites (Figure 4) increases YX phase in the anomalous phase areas (Figure 3). However, the true resistivity distribution around the Kitakami Lowland is difficult to obtain based on the present data because the shallow resistivity distribution is not constrained in the blank area of MT stations, as we discussed previously.

The aftershocks are dominantly distributed in the resistive zone but are slightly within the C-1 and C-2 conductors. Because these are interpreted as granitic and Tertiary sedimentary rocks and high-temperature areas, respectively, the aftershocks occurred in brittle areas but rarely in ductile areas. This indicates that the seismicity depended highly on three-dimensional elastic heterogeneity. As mentioned in the ‘Introduction,’ the magnitude and rupture area of the 2008 Iwate-Miyagi Nairiku earthquake (M 7.2) are anomalously large for an earthquake occurring in a volcanic area where ductile zones are generally distributed. However, this study has indicated that the ductile zones related to volcanic activities are patchily distributed and that the size of the brittle area is large enough for M 7-class earthquakes to occur. These elastic heterogeneities may also have been responsible for the earthquake occurrence in a different way because elastic heterogeneities may result in local stress concentration zones and can cause faulting (e.g., Ichihara et al. 2008, 2013; Iio et al. 2002). These interpretations imply that the MT method can detect elastic heterogeneities that may control the occurrence and magnitude of the large inland earthquakes. Therefore, three-dimensional resistivity modeling based on MT surveying is important for understanding earthquake occurrences.


We conducted magnetotelluric surveys at 14 stations around the focal area of the 2008 Iwate-Miyagi Nairiku earthquake (M 7.2). Based on the MT impedances along four profiles by the present and previous studies, a preliminary 3-D resistivity model was obtained using WSINV3D code. The resistivity model showed a shallow conductive zone (C-1) and a few distinct conductive areas around the focal area (C-2, C-3a, C-4, and C-5). C-1 was interpreted as Tertiary sediment based on its geological distribution. C-2 and C-3a possibly indicate high-temperature zones related to volcanic activities beneath Mt. Kurikoma and Onikobe Caldera. Aftershocks were distributed mainly in the resistive zone and not in the aforementioned conductive zones, which implies that elastic heterogeneity due to volcanic activity and geology may control the magnitude and occurrence frequency of such earthquakes. However, this study could not constrain the precise resistivity distribution in the blank areas of MT stations. Thus, dense surveys between the existing profiles of MT stations are required for more detailed interpretations.



We thank the landowners in the study region for their permission to establish observation sites on their land. H. Shinohara of Akita University provided assistance with the data acquisition. The Nittetsu Mining Consultants Co., Ltd. provided us with their continuous geomagnetic records at the Sawauchi station as remote references. The Geographical Survey Institute provided the MT impedance at the Esashi station. Prof. Okada, Graduate School of Science, Tohoku University, provided the seismicity data. Generic Mapping Tools software (Wessel and Smith 1998) was used to draw some of the figures. The manuscript was improved by thoughtful comments from two anonymous reviewers. This research was supported by the Grant-in-Aid 20900001 (Kaken-hi) and the Multidisciplinary Research Project for High Strain Rate Zones of the Ministry of Education, Culture, Sports, Science and Technology (MEXT), Japan.

Authors’ Affiliations

Research and Development Center for Earthquake and Tsunami, Japan Agency for Marine-Earth Science and Technology
Earthquake Research Institute, The University of Tokyo
Faculty of International Resource Sciences, Akita University
Research Center for Prediction of Earthquakes and Volcanic Eruptions, Graduate School of Science, Tohoku University
Volcanic Fluid Research Center, Tokyo Institute of Technology
Institute of Geology and Geoinformation, National Institute of Advanced Industrial Science and Technology (AIST)
Institute of Seismology and Volcanology, Graduate School of Science, Hokkaido University
JGI, Inc.


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