High resolution seismic velocity structure around the Yamasaki fault zone of southwest Japan as revealed from travel-time tomography
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2013
Received: 4 August 2012
Accepted: 13 December 2012
Published: 17 September 2013
The Yamasaki fault zone in southwestern Japan currently has a high potential for producing a large damaging earthquake. We carried out a seismic tomographic study to determine detailed crustal structures for the region. The velocity model clearly images a low-velocity and high V p /V s (high Poisson’s ratio) anomaly in the lower crust beneath the Yamasaki fault zone at a depth of ~15–20 km. This anomaly may be associated with the existence of partially-melted minerals. The existence of this anomaly below the fault zone may contribute to changing the long-term stress concentration in the seismogenic zone.
Key wordsYamasaki fault travel-time tomography velocity structure
The Yamasaki fault zone is one of the seismically most active onshore faults in southwestern Japan. This tectonic feature is a left-lateral active fault zone with a length of approximately 80 km running northwest to southeast from Okayama to Hyogo Prefectures. Damaging earthquakes have not occurred for about 1100 years, and the largest recent event was a M 5.6 event on May 3, 1984, near the Kuresaka-Toge fault.
The level of small earthquakes is relatively high in the Yamasaki fault zone, with about 3000 M 0.0 to M 3.0 occurrences per year. Previous studies show that the seismic activity of the region appears to have a periodicity of 5–6 years, and, since 2001, activity appears to have migrated toward the southeast along the fault zone (Nakao et al., 2004) around the Kuresaka-Toge, Yasutomi, and Biwako faults. Watanabe et al. (1996) investigated the crustal movement around the Yamasaki fault zone after the 1995 Mw 6.9 Kobe (Hyogo-ken Nanbu) earthquake, located about 50 km to the southeast. They showed that the seismicity of the Yamasaki fault zone became active after the occurrence of this earthquake, while the areas outside the fault zone did not show any significant increase, suggesting that an active fault is sensitive to the crustal stress concentration. The Yamasaki fault zone is an onshore active fault that has the potential to generate a large earthquake and cause severe damage. Therefore, the study of the physical properties of this fault for the purposes of earthquake hazard mitigation is very important.
Previous tomographic studies in other regions of Japan have showed varied results concerning the relationship between earthquake source regions and the seismic velocity structure. For example, Zhao et al. (1996) reported a low seismic velocity and a high Poisson’s ratio anomaly around the hypocenter of the 1995 Kobe earthquake. They showed that this anomaly may be due to high pore fluid pressure and a fluid-filled, fractured rock matrix near the bottom of the seismogenic layer that contributed to the initiation of the Kobe earthquake. Shibutani et al. (2005) showed the relationship between the source process of the 2000 western Tottori earthquake and the three-dimensional velocity structure. They found that the slip is small for the high-velocity regions and large in the shallow low-velocity regions, and concluded that crustal structure heterogeneity could control the rupture process of the mainshock. A tomographic study of the 2004 mid-Niigata prefecture earthquake by Okada et al. (2005) concluded that the high-velocity area with low V p /V s values, imaged in the footwall, was considered to be old basement rock, while, the low-velocity areas with high V p /V s values in the hanging wall were associated with sediments. Nakajima et al. (2006) investigated the major features of the complex seismic velocity structure around the Nagamachi-Rifu fault in northeastern Japan, with implications for the existence of fluid-rich regions in the mid to lower crust as indicated by low velocity and high Poisson’s ratio anomalies.
Previous regional tomographic studies in southwestern Japan include Nakajima and Hasegawa (2007), which focused on the deep magma source beneath the Chugoku district and the deep structure beneath the Kii Peninsula. Another study by Matsubara et al. (2008) constructed seismic velocity structures for the entire Japan Islands with a unified resolution. However, these studies do not focus on the crustal structure around the Yamasaki fault zone. In this study, we report the results of high-resolution travel-time tomography using a large data set obtained by a dense seismic network. The analyses of this large data set enables resolution of the details of the regional velocity structure that have not been previously recognized; in particular, low-velocity zones and regions of high V p /V s . The purpose of the study is to examine detailed crustal structures in, and around, the Yamasaki fault and its relation to the process of large earthquake generation.
2. Data and Methods
We used the SIMULPS12 method (Eberhart-Phillips, 1993; Evans et al., 1994) which provides a local earthquake algorithm inversion to calculate simultaneously the 3-D V p and V p /V s structure and hypocentral adjustments. Predicted arrival times through the 3-D structure are calculated for ray paths using the pseudo-bending technique of Um and Thurber (1987). Since the S data are fewer in number and, generally, of lesser quality than the P data, the calculation of V p /V s using S-P times rather than from separate estimates of V s and V p is usually more robust (Eberhart-Phillips, 1993). We used grid nodes spaced at 10 km in the horizontal direction and 2–3 km in the vertical direction for the tomography inversion, as shown in Fig. 1(a). The initial V p and V p /V s models for the tomographic model are from Shibutani et al. (2008).
3. Model Resolution
4. Seismic Tomographic Images
Summary of the features of four anomalies beneath the Yamasaki fault.
Moderate to high
V p /V s
Moderate to high
Moderate to high
In the shallower part of the crustal structure from the surface to 5-km depth below the Hijima fault, there is a region of low V p and low V s that coincides with low V p /V s and low PR (Anomaly 1). This is seen in the Line-3 cross-section of Fig. 6. There is a similar region of low velocity at a shallow depth beneath the Kuresaka-Toge fault; however, the V p /V s is moderately high (Anomaly 2), as seen in Line-6.
In general, we observe high V p /V s ratios and high PR in the regions beneath the Yamasaki fault zone (Fig. 6) at depths of ~15–17 km. At depths of 15–20 km beneath the Hijima fault, there are prominent low velocities (low V p and low V s ), high V p /V s , and high PR. These can be clearly seen in Line-4 of the cross-sections in Fig. 6 (Anomaly 3). At depths of 15–20 km beneath the Kuresaka-Toge fault, there is a region of moderately high V p , low V s anomaly, with high V p /V s and high PR (Anomaly 4). This can be seen in Line 6 of Fig. 6.
Seismic velocities and Poisson’s ratios vary in crustal rocks depending on factors such as pressure, temperature, composition, crack density, and fluid content. A laboratory study by Takei (2002) showed that the effect of fluids on seismic velocity depends on the type of fluids, such as melt-filled pores, or water-filled pores, as well as the shape of the fluid-filled pores. The existence of melt-filled pores decreases seismic velocity and increases PR. The melt-filled pores are independent of the shape of the pores. On the other hand, water-filled pores have a different effect on seismic velocity and PR, which depends on the shape of the pores (Takei, 2002). Water-filled pores of a small aspect ratio decrease seismic velocity with increasing PR, which is the same effect as for melt-filled pores. Water-filled pores of a large aspect ratio, however, can lower PR slightly with decreasing seismic velocity.
In the upper crust, low V p , low V s and low V p /V s (low PR) regions are imaged beneath the Hijima fault, as evidenced by Anomaly (1) in Fig. 7, while the region beneath the Kuresaka-Toge fault shows moderately high V p /V s (moderately high PR) as shown by Anomaly (2). Our interpretation is that the low velocities and low V p /V s values of the shallow crust beneath the Hijima fault may be attributed to the existence of water-filled pores of relatively large aspect ratio, while the low velocities and moderate high V p /V s values beneath the Kuresaka-Toge fault may be due to the existence of water-filled pores of a relatively small aspect ratio (e.g., Takei, 2002; Matsubara et al., 2004; Kato et al., 2006; Nakajima et al., 2006).
In the lower crust, there is a prominent region beneath the Hijima fault at ~17-km depth with low V p , low V s , high V p /V s of ~1.75–1.8, and a high PR of ~0.26–0.28 region, as marked by Anomaly (3) in Figs. 7 and 8. Such anomaly features have been commonly imaged in the lower crust in northeastern Japan from previous travel-time tomographic studies (e.g., Nakajima et al., 2001, 2006; Nakajima and Hasegawa, 2003; Kato et al., 2006; Matsubara et al., 2008) and they are interpreted to be possibly related to partially molten materials. Although Quaternary, or active, volcanoes are not found around the Yamasaki fault zone, Yoshida (2001) showed that temperatures in the lower crust generally exceed the wet solidus of basalt and andesite. The existence of an aseismic Philippine Sea slab beneath Chugoku has been found by analyzing ScSp phases (Nakanishi, 1980) and by the receiver function studies of Ueno et al. (2008) and Shiomi et al. (2008). Partially-melted materials in the lower crust may be associated with upwelling processes in the mantle wedge above the slab. A regional seismic study (Nakajima and Hasegawa, 2007) also imaged a low-velocity anomaly beneath the Chugoku region. Therefore, partial-melt minerals in the lower crust might be causing Anomaly (3) in this study.
Anomaly (4) in the lower crust at a 17-km depth beneath the Kuresaka-Toge fault in the southeastern part of the Yamasaki fault zone exhibits contrasting properties for P and S waves (moderately high V p and low V s ) with a high V p /V s of 1.76–1.8 and a high PR of about 0.26–0.28. Such features are difficult to explain by the presence of water and/or melt-filled pores. One plausible explanation is the existence of anhydrous plutonic rocks in this region (Yoshida, 2001), however, this interpretation needs further investigation. The presence of partial melt or fluids beneath the seismogenic zone in the lower crust structure can change the deformation of the fault zone and affect its stress accumulation (Zhao et al., 1996; Hasegawa et al., 2000, 2005; Nakajima et al., 2006).
Low V p /V s values are imaged in the areas where active small earthquakes frequently occur in the Yamasaki fault zone. The low to moderately-high V p /V s zone for seismicity clusters are also observed in southern California, and Lin and Shearer (2009) suggested the presence of water-filled cracks with porosities of several percent.
Using a high-resolution travel-time tomographic inversion, we have successfully determined the three-dimensional V p , V s , V p /V s ratio and PR structures to identify crustal heterogeneity around the Yamasaki active fault system. The structure in this region has previously not been studied in such detail. These new results of low velocities and low V p /V s regions in the upper crust at depths down to 5-km below the Yamasaki fault zone, are interpreted as regions of water-filled pores with relatively large aspect ratio. Also, low velocities and high V p /V s regions observed in the lower crust at depths of 15–20 km beneath the Yamasaki fault zone may be associated with the existence of partially-melted minerals. The existence of these low-velocity regions may affect the long-term strength of the fault zone and change the stress concentration in the seismogenic zone.
We thank the Tottori and Abuyama Observatories of the Disaster Prevention Research Institute, Kyoto University, the University of Tokyo, National Research Institute for Earth Science and Disaster Prevention (NIED), National Institute of Advanced Industrial Science And Technology (AIST), Ministry of Education, Culture, Sports, Science, and Technology, Japan (MEXT), and the Japan Meteorological Agency for providing earthquake arrival-time data. We thank the anonymous reviewers for their constructive comments which significantly improved the paper.
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