SCG62-01

Room:303

Time:May 27 14:15-14:30

Repeating Shallow Slow-Slip-Events along the Block Boundary in the Northern Hokkaido
IKEDA, Shohei1∗ ; HEKI, Kosuke2
1

Department of Natural History Sciences, Graduate School of Science, Hokkaido University, 2 Department of Natural History
Sciences, Faculty of Science, Hokkaido University
In Northern Hokkaido, to the north of Rumoi, earthquakes larger than M6 class have not occurred for a few decades. However,a block boundary is considered to run N-S in this region with the E-W convergence rate of about 1 cm/year coming from theeastward movement of the Amurian Plate (Loveless and Meade, 2010). Ohzono et al. (2014) reported the shortening of thebaseline between Horonobe and Nakatombetsu of about 1cm over 4 months period from 2012 summer to the early 2013 and they
considered it an inland SSE (slow slip event).
In this study, we thought there might have been other SSEs at different segments along the block boundary, and analyzed timeseries of distances between GEONET GNSS points that cross this block boundary from Wakkanai (north) to Rumoi (south). The
baseline between Nakagawa and Otoineppu, about 20 km to the south of Horonobe-Nakatombetsu, was found to have shortenedby a few millimeters in the middle 2005 and middle 2007. We also found that the distance between Haboro and Horokanai,
further south, also decreased in late 2002 and early 2004. All these contractions were a few millimeters and took 1-2 months.
To detect changes objectively, we followed Nishimura et al. (2013), and monitored the differences in AIC (Akaike’s Information
Criterion) between the two cases, i.e. regression with SSE and without SSE. We considered an SSE occurred when AIC significantly decreased by assuming an SSE.
Shallow seismicity occurs along the N-S block boundary in the northern Hokkaido. The seismic zone bends and runs E-W at
the latitude of Rumoi (44.1N), and is connected to the plate boundary along the eastern margin of the Japan Sea.In Rumoi, an M6
class earthquake occurred in December, 2004 with over twenty aftershocks larger than M3 (Takahashi and Kasahara, 2005). In
this region, more earthquakes occur than in the region to the north. In conclusion, block convergence would take place as regularearthquakes in the region to the south of Rumoi. On the other hand, the convergence will be occurring as repeating SSE to thenorth of Rumoi.

Keywords: Northern Hokkaido, inland, SSE, GPS, GNSS

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SCG62-02

Room:303

Time:May 27 14:30-14:45

Estimation of fault parameters of slow slip event, off the Kii Peninsula, detected byDONET
SUZUKI, Kensuke1∗ ; NAKANO, Masaru1 ; HORI, Takane1 ; TAKAHASHI, Narumi1
1

JAMSTECThe Japan Agency for Marine-Earth Science and Technology (JAMSTEC) installed permanent ocean bottom observation stations named as Dense Oceanfloor Network System for Earthquakes and Tsunamis (DONET) off the Kii Peninsula to monitor
earthquakes and tsunamis. We derived the component of sea floor change from the ocean-bottom pressure record, and we detected the ocean-bottom pressure changes, starting from February 2013, at a part of stations deployed to DONET (Suzuki etal., 2014). These pressure changes were synchronized with a decrease in the background seismicity within the area of a nearby
earthquake cluster. Although we considered that these pressure changes show the vertical sea floor changes due to the crustal
deformation caused by slow slip event (SSE), we did not estimate the fault parameters of SSE. Therefore in this study we tried
to estimate the parameters of the fault slip that caused crustal deformation.
In this study we estimated the fault parameters of SSE by comparing the observed vertical displacements with ones calculatedby the fault model using the dislocation source solutions (Okada, 1992). In Suzuki et al. (2014), we derived the vertical crustal
deformations from the ocean-bottom pressure changes as described below. First we removed the tidal component from the oceanbottom pressure records by BAYTAP-G (Tamura et al., 1991). Next we subtracted the average of pressure change taken over therecords at stations connected to each science node from the records removed tidal component in order to remove the pressurechanges due to atmosphere pressure changes and non-tidal ocean dynamic mass variation. Therefore in this study we subtracted
the average changes from the each theoretical displacement when we calculated the theoretical displacements by using the fault
model.
Although there are nine parameters in the fault model, we observed vertical displacements at only four stations. Therefore wecannot uniquely determine the fault parameters, and we need to constrain the fault parameters in the inversion process. In thisstudy we supposed the plate boundary and splay fault in the sedimentary wedge as the fault that caused crustal deformation. In
the plate boundary case, we fixed the strike, dip and rake, and estimated other parameters by grid search method. However wemade the fault depth to be coincident with the plate boundary depth. On the other hand in the splay fault case, we estimatedthe fault depth and dip by the grid search method in addition to parameters estimated in the plate boundary case. However fault
depth was constrained in the shallower part than the plate boundary depth.
Although we explain the relative vertical displacement pattern in the plate boundary case, the average displacement taken overthe stations is large. If this large average displacement actually occurred, we could detect it from the pressure gauge records
removed tidal component. Therefore it is difficult to explain the observed displacements by using the fault model along the plateboundary. On the other hand in the splay fault case, the average displacement is small and the calculated relative displacement
pattern is coincident with observed one. Therefore the splay fault case is more reasonable to explain the observed vertical displacements. In the future we will consider the fault model having other type mechanisms and investigate the relationship between
the fault slip and the seismicity change.

Keywords: DONET, ocean bottom pressure change, slow slip event, seismicity change

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SCG62-03

Room:303

Time:May 27 14:45-15:00

Robust estimation of spatio-temporal distribution of slow slip event by switching model
ARAKI, Takamitsu1∗ ; OCHI, Tadafumi1 ; MATSUMOTO, Norio1 ; AKAHO, Shotaro1
1

National Institute of Advanced Industrial Science and Technology

Short-term slow slip event (SSE) can be precisely captured by only highly sensitive instruments such as borehole strainmeterand tiltmeter, Meanwhile, since such sensitive instruments is affected by various external factors, the observed data contain large
noise which has complicated structure in time.
We estimate the spatio-temporal distribution of SSE by analyzing noisy data such as strain data and tilt data. Conventionally,
the Network Inversion Filter (NIF) has been widely used to estimate the spatio-temporal distribution of the larger SSE, e.g., longterm SSE, based on smaller noise data such as Global Navigation Satellite System (GNSS). However, since the NIF assumes thesame dynamics of the noise and slip signals over the entire observation period, the NIF cannot eliminate the large noise signals
from such noisy data. Therefore, the NIF cannot correctly estimate SSE from the entire period of the noisy strain and tilt data.
We propose the estimation method using the switching model that represents three forms in three periods. In the first period,
the fault never slips, in the second period, the fault is slipping slowly, and in the third period, the fault is being at rest. The time
points at which the model changes as well as the parameters of the switching model are estimated by the maximum likelihood
method using the Expectation-Maximization (EM) algorithm. The EM algorithm maximizes the likelihood with little dependency
on initial parameters and enables us to estimate the parameters stably. The spatio-temporal distribution of SSE is estimated using
the Kalman filter, after the model changing time points and the parameters of the model are estimated. The strict and physicallyreasonable assumptions of the fault slip in first and third periods remove the almost noise signal in the periods, and lead to thestable estimate of the fault slip in the second period.
In order to compare the proposed method to the NIF, we applied the proposed method and the NIF to the noisy synthetic data
and the strain data. The synthetic data were produced by the simulation of SSE and large noise signals, and the strain data were
measured in the Tokai and Kii area, central Japan, on 2012. In the synthetic data, the fault slip estimated by the proposed method
is much more accurate than that by the NIF. The proposed method also estimated the more reasonable SSE than the NIF in thestrain data. It is important to detect the starting time point of SSE without any information, and the proposed method correctly
detected the starting time point of SSE in both data sets, which the NIF could not capture.
Keywords: Slow slip event, Strain data, Switching model, Maximum likelihood method, Kalman filter

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SCG62-04

Room:303

Time:May 27 15:00-15:15

An attempt to estimate duration for short-term SSEs in southwest Japan using the stacking
method of GNSS data
NISHIMURA, Takuya1∗ ; MATSUZAWA, Takanori2 ; KIMURA, Takeshi2 ; OBARA, Kazushige3
1

Disaster Prevention Research Institute, Kyoto University, 2 National Research Institute for Earth Science and Disaster Prevention, 3 Earthquake Research Institute, The University of Tokyo
Introduction
Short-term slow slip events (SSEs) with duration of several to ten days occur on a subducting plate interface in southwest
Japan. Nishimura et al. (2013) and Nishimura (2014) suggest that short-term SSEs occur not only in a deep part (20 ∼ 40 kmdeep) from the Tokai region to the Bungo Channel but also along the Ryukyu trench from Hyuganada to the Yaeyama Islands.
Because displacement signal caused by short-term SSEs is comparable to a noise level of GNSS data, Nishimura et al.(2013)
assumed no duration of short-term SSEs and fitted an instantaneous step function with a linear trend to GNSS time-series toestimate a fault model. It is unclear how long the detected SSEs continue.
It is a gap of duration between short-term and long-term SSEs in southwest Japan. Intermediate-term SSEs with duration of
one or two months have never been reported. This gap may be artificial due to less sensitivity of observation sensors including
GNSS, strainmeters, and tiltmeters to the signal for those periods.
In this study, we try to estimate duration of short-term SSEs using a combination of the detection method of short-term SSEs
using GNSS data (Nishimura et al., 2013) and the stacking method for the detection of crustal deformation (Miyaoka and Yokota,2012).
Data and Analysis
The used data are daily GNSS coordinates (F3 solution) published by the Geospatial Information Authority of Japan. We
detected short-term SSEs and estimated their fault models using the method of Nishimura et al.(2013) and Nishimura (2014).
And then, we applied the stacking method (Miyaoka and Yokota, 2012) for GNSS time-series using the displacement calculated
from the fault model. The detailed procedure of the stacking follows. First, we select a time window of 181 days centering adate of a short-term SSE in NS and EW components of GNSS time-series. We removed a linear trend and calculated RMS (RootMean Square) using the data in the time window excluding the middle 60 days. The RMS is used as the noise level of the data
and the time-series is normalized by the noise level. Next, we calculate signal to noise ratio (SNR) every component of GNSS
stations using the noise level and the signal calculated from the fault model. Then, we stack the normalized time-series in orderof SNR and calculate the noise level of the stacked time-series. We stop stacking when the SNR of the stacked time-series is thehighest. Finally, we estimate the duration of the short-term SSEs by fitting a lamp-type function to the stacked time-series.
ResultStacking 30 ∼ 100 time-series gives the highest SNR for the short-term SSEs along the Nankai Trough. Although it is difficult
to recognize transient signals of SSEs in the original time-series, we can visually inspect duration of SSEs using the stacked
time-series, which demonstrates effectiveness of the stacking method. The estimated duration for SSEs with good SNR timeseries ranges several days to a month approximately. It is longer than that estimated in the previous studies (e.g., Sekine et al.,2010) in some cases. Although such a long duration can be explained by misrecognition for two succeeding SSEs with a shortinterval, the long duration may be real in some cases. We also report a regional feature of duration, comparison with an activityof low-frequency tremors and Hi-net tilt data by the National Research Institute for Earth Science and Disaster Prevention.
Acknowledgements We thank the Geospatial Information Authority of Japan for providing the daily coordinates of the
GEONET stations (F3 solutions).
Reference
Miyaoka, K., and T. Yokota (2012), Zisin, 65, 205-218.
Nishimura, T., T. Matsuzawa, and K. Obara (2013) JGR Solid Earth, 118, 3112-3125.
Nishimura, T. (2014) PEPS, 1:22.
Sekine, S., H. Hirose, and K. Obara (2010) JGR Solid Earth, 115, B00A27.
Keywords: Slow Slip Event, GNSS, Southwest Japan, Duration

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SCG62-05

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Time:May 27 15:15-15:30

Slow slip event within a gap between tremor and locked zones in midwestern Shikoku
TAKAGI, Ryota1∗ ; OBARA, Kazushige1 ; MAEDA, Takuto1
1

Earthquake Research Institute, UTokyo

Episodic tremor and slip (ETS), a slow slip phenomenon on the plate interface, occurs at downdip region of seismically lockedzone in the Nankai subduction zone. The locked zone has potential to be ruptured by great earthquakes. However, there is a gap
between ETS and the locked zones. In the present study, we detected a slow slip event (SSE) within the gap from GNSS data by
subtracting steady state component and postseismic effect of large earthquakes.
We analyzed GNSS daily coordinates at GEONET stations in southwest Japan provided by GSI. After removing offsets due tolarge earthquakes and equipment repairs, we applied the spatial filtering proposed by Nishimura et al. (2013) to reduce spatiallycoherent noise. Then, we estimated trend and seasonal components from the displacement time series during two years from2007 to 2008, and subtracted those from entire time series. The displacement field after 2011 contains short wavelength variation
at midwestern Shikoku in addition to long wavelength variation due to the postseismic effect of the 2011 Tohoku-Oki earthquake.
Thus, we estimated the long wavelength variation from the displacement data without midwestern Shikoku by assuming the longwavelength variation as a bivariate quadratic function of horizontal space. Finally, subtracting the estimated long wavelengthvariation from displacement filed, we extracted the short wavelength variation.
The short wavelength variation in midwestern Shikoku shows displacements toward southeast and it may be attributed to athrust fault slip in the plate convergence direction. Modeling with a rectangle fault using the equation by Okada (1992) reveals
that a dip slip of 2 cm/year within the gap between ETS and the locked zones well explains the observed displacements. The
dip slip event lasts at least 1.5 years. The rectangle faults estimated from annual displacements for the periods starting from
Apr. 2011, Oct. 2011, Apr. 2012, and Oct. 2012, are located between mid Shikoku and the Bungo channel with dimensionsof 150-180 km length and 20-40 km width. The strikes of the faults are almost parallel to isodepth contours of the subducting
plate. A similar SSE is detected in 2004 and 2005, which was partly reported by Kobayashi (2010), while the fault length of the
2004-2005 event is shorter than that of the 2011-2012 event. These SSEs within the gap follow the 2003 and 2010 long-term
SSEs in the Bungo channel and are located just east of the long-term SSEs. Therefore, after the long-term SSEs in the Bungo
channel, the slip may migrate east and small slip last within the gap between ETS and the locked zones.
Tremor in western Shikoku occurs at intervals of about a half years, and migrates along the strike direction with durations of afew days to a week. After 2011, the migration pattern has been changed. Some episodes show migrations with length longer than
120 km, while such long migration has not been observed before 2011. Since the long-term SSE detected by the present study islocated shallow part of the tremor episodes with the long migration, it is suggested that the shallower long-term SSE facilitates
the migration of the deeper short-term SSEs.
In Cascadia subduction zone, there is also a gap between ETS and locked zones. Understanding slip behavior in the gap zone isof importance for estimating downdip limit of grate earthquake rapture (Hyndman, 2013) and understanding stress accumulation
for great earthquake (Wech and Creager, 2011; Yokota and Koketsu, 2015). In the present study, we detected the long-term SSE
within the gap from GNSS data by removing trend components and postseismic effects of large earthquakes. We suggest that,between ETS and the locked zones, the long-term SSE slowly releases accumulated strain due to plate convergence.

Keywords: slow slip event, slow earthquake, GNSS, non-volcanic tremor, subduction zone

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SCG62-06

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Time:May 27 15:30-15:45

The properties and variations of repeating slow slip events near Hateruma Island, southwestern Japan
TU, Yoko1∗ ; HEKI, Kosuke1
1

Department of Natural historical sciences, Hokkaido University

Slow slip events (SSEs) are a kind of transient motion related to slow fault rupture at the plate interface (Heki and Kataoka,2008). These events are classified into slow earthquake series due to their long periods than regular earthquakes. SSEs are usually detected on intensely coupled plate boundaries such as Cascadia subduction zone (Dragert et al., 2001), Alaska (Ohta et al.,2007) and central Japan (Ozawa et al., 2002, 2003). For this reason, SSEs are considered to relate to large thrust earthquakes andcan be evidence for seismic coupling on subduction zones. However, in the southwestern Ryukyu trench where most researchers
believe that it should be a creeping and aseismic plate boundary. Nevertheless, Heki and Kataoka (2008) identified more than 20
SSEs near Hateruma Island using ten-yrs GNSS (Global Navigation Satellite Systems) data and found that repeated intervals areapproximately 6 months regularly. Moreover, the events occurred at a fault patch that is as deep as 20 to 40 km, and their releaseseismic moments are Mw 6.6 on average. In addition, Nakamura (2009) identified a slow crust deformation near Yonaguni Islandthat was induced by an Mw7.1 earthquake, and the duration of this event is longer than 5 yrs. These phenomena describe that thesouthwestern Ryukyu subduction zone could be a coupled plate boundary and have potentials to cause large thrust earthquakes.
In order to understand the properties and variations of SSEs in this area, GEONET GNSS daily coordinate solutions of 16-yrs(1997-2014) are used in this study. During this period, a total of 33 SSEs are identified from Hateruma station through visualinspection. The average recurrence interval (6.3 mos) and the average release seismic moment (Mw 6.6) consistent with theresults of Heki and Kataoka (2008). However, the interval and slip of SSEs vary in a short time. For instance, from 2005 to 2007,
the interval decreases suddenly from 6 to 4.5 mos without specific causes, and then turns back to the previous level. Moreover,the slip rate (cumulative slip/ lapse time) of SSEs in this area is 8 cm/y on average. From 1997 to 2001, the slip rate is 10 cm/y;and during 2003 to 2006, the slip rate increases slightly to 11 cm/y. Afterward, between 2007 to 2013, it drops remarkably to 6
cm/y, and then increases again to 12 cm/y near the end of 2013.
Although the slip rate significantly increases in 2002 and 2013, the mechanisms of the variations are still uncertain. For thisissue, Heki and Kataoka (2008) indicated the slip rate variation of SSE in 2002 could relate to nearby large earthquakes (Mw>7). Subsequently, Nakamura (2009) calculated the 4CFS on the fault of SSEs and proposed the slow crust deformation near
Yonaguni Island induced by one thrust earthquake might affect the slip rate variation. However, above idea cannot explain theslip rate change in 2013, since no significant earthquake occurred near the southwestern Ryukyu trench in this period. On thecontrary, one earthquake swarm activity in the Okinawa trough, approximately 50km north of the SSE fault patch, started simultaneously. On the basic of displacement data of Yonaguni and Hateruma stations, we infer that the earthquake swarm was
generated by a dyke intrusion which relates to the Okinawa trough spreading. Through Coulomb failure stress calculation, thepositive 4CFS confirms the dyke intrusion triggered the slip rate change of SSEs in 2013.
Keywords: SSEs, Hateruma Island, variations, Ryukyu subduction zone

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SCG62-07

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Time:May 27 15:45-16:00

The Apr 2013 earthquake swarm and dyke intrusion in the Okinawa troughANDO, Masataka1∗ ; IKUTA, Ryoya2 ; TU, Yoko3 ; CHEN, Horng-yue4 ; LIN, Cjeng-horng4
1

Center for Integrated Research and Education of Natural Disasters, 2 Graduate School of Science, Shizuoka University, 3 Departmentof Natural Historical Sciences, Hokkaido University, 4 Institute of Earth Sciences, Academia Sinica
In April 2013, a shallower earthquake swarm occurred in the Okinawa trough, 50 km NNE of Yonaguni Island, following morethan 10 yrs of seismically quiet period in the area. The major seismic activity decayed within a week. During the period, 28
earthquakes of Mw >4.5 (max Mw 5.2) occurred. The sum of all seismic moments is equivalent to Mw 5.7. GPS data from sevenstations from GEONET and three from Taiwan are used over a sufficient long interval of dataset. During the active period, crustal
displacements reached 4.7 cm in SSW direction on Yonaguni Island, 1cm in the E direction on Iriomote, sub-cm on Ishigaki andother islands and no noticeable displacements at stations in Taiwan.
A kinematic GPS analysis of theses data reviles that this deformation started at the time of the earthquake swarm and slowly
continued over two days. During the period no step-like movements exceeding a threshold level occurred, suggesting the absenceof sudden slips at the earthquake source area. We propose two source models to interpret these GPS data, 1) a normal fault of
Mw 7.0 and 2) a magma intrusion with the thickness of 3 m. These models cannot be distinguished from the GPS data alone.
Prior to the earthquake swarm, the GPS velocity vector at Yonaguni is 6.5 cm/yr in the SSE direction but that increases at 8.4
cm/yr after the earthquake swarm and furthermore 9.5 cm/yr throughout 2014. The long-lasting and accelerating GPS displacements suggest a strong preference for the dyke intrusion model.
A question may arise whether such magma intrusion causes the rifting of the Okinawa trough and hence the southward migration of the Ryukyu arc. To solve the question, the data from the baseline of Iriomote and hateruma islands is critical. Thisbaseline is aligned perpendicular to the general trend of the western Ryukyu trench. The baseline of 40 km between the twoislands shows a constant extension of 1 mm/yr from 2001 to 2015. The long-term and steady extension of the baseline suggeststhat rifting of the Okinawa trough is caused by the retreat of the Ryukyu trench due to a rollback of the Philippine Sea plate in
the western Ryukyu trench.

Keywords: earthquake swarm, normal fault, Okinawa trough, back-arc rifting, dyke intrusion, Ryukyu trench

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SCG62-08

Room:303

Time:May 27 16:15-16:30

Correlation of activity of very low frequency earthquakes with tide in the Ryukyu Trench
NAKAMURA, Mamoru1∗ ; KAKAZU, Keito1
1Faculty of Science, University of the Ryukyus

Recently, very low frequency earthquakes (VLFEs) were observed in the shallow part of the Ryukyu subduction zone (Andoet al. , 2012; Asano et al. , 2013, 2014, 2015; Nakamura and Sunagawa, 2015). Since the stress drop of the VLFEs are very small
comparing with that of ordinary earthquake (Ito and Obara, 2005), the VLFEs would be activated by small stress change such as
tidal stress. Then we investigated the activation of the VLFEs by earth tide.
We used the events (Mw>3.5) which occurred from January 1, 2002 to December 31, 2014. We employed the VLFE catalogue
which is determined by manually-picking method (Nakamura and Sunagawa, 2015). We employed the ocean-tide data at Naha,
Ishigaki, and Naze which is installed by Japan Meteorological Agency. Then we computed the theoretical horizontal strain by
the earth tide and ocean loading using GOTIC2 (Matsumoto et al., 2001) to compare the theoretical strain and activity of the
VLFEs.
First we selected five areas along the Ryukyu Trench where the VLFEs are clustered, then we counted the number of VLFEs
as a function of the phase of ocean tide. The VLFEs had been activated at low tide, and they had been quieted at high tide in allareas excluding southwest of Ryukyu. Moreover, the activation occurred on the compressional stage by the earth tide and ocean
loading, and quiescence occur on the tensional stage. The VLFEs were activated when the shear stress on the plate interface
reached maximum.
Since the VLFEs in the Ryukyu Trench are thrust type or reverse fault type (Ando et al ., 2012), the VLFEs would be activatedin the compressional shear stress stage. This suggests that the activity of the VLFEs is triggered by stress change by the earth
tide. The amplitude of the shear stress on the plate interface is large in the central and north Ryukyu Trench but it is small inthe southwestern Ryukyu Trench because of the strain by the ocean loading and strike of the Ryukyu Trench. This generates thedifference in activation of VLFE by the ocean tide along the north-central and southwestern Ryukyu Trench.

Keywords: very low frequency earthquake, tide, Ryukyu Trench

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SCG62-09

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Time:May 27 16:30-16:45

Tidal sensitivity of tectonic tremors in subduction zones
YABE, Suguru1∗ ; TANAKA, Yoshiyuki2 ; HOUSTON, Heidi3 ; IDE, Satoshi1
1

EPS, UTokyo, 2 ERI, UTokyo, 3 ESS, Univ. of Washington

Tectonic tremor, which is one of slow earthquakes occurring in subduction zones, have been known to be triggered by small
stress perturbation such as passing surface wave from distant earthquake and tidal stress. Tidal sensitivity of tremors can bedetected by investigating the frequency of tremor catalog, but more quantitative comparison gives us useful information. By
comparing tremor activity with calculated tidal stress on the plate interface, some previous studies estimate frictional propertyon the plate interface, such as frictional parameter in rate and state friction (Tanaka et al., 2008), friction coefficient (Thomas etal., 2012; Houston, 2015). Furthermore, recent studies reveal the relation between tremor rate and tidal stress is exponential (Ideand Tanaka, 2014, Houston, 2015), which would represent the frictional property of plate interface. However, the analyses ofprevious studies are limited to specific places in subduction zones. Hence in this study, we try to estimate the spatial variation of
tidal sensitivity in Nankai, Cascadia and Mexican subduction zones.
Tidal stress calculation includes both body tide and ocean tide. Tidal stress is converted to normal stress and shear stress on
the plate interface based on the local plate model and plate movement.
Tremor catalog is from Yabe and Ide (2014). We calculate tremor rate at each tidal stress level following Ide and Tanaka(2014) and Houston (2015). Tidal sensitivity is calculated from this data using maximum likelihood method. The uncertainty of
estimated parameter is assessed as well.
In this study, we categorize tremors in the catalog into four types. Tremors occurring between major ETS episodes are
categorized into inter-ETS events. Tremors in ETS events are categorized into three categories (”early”, ”front”, and ”later” as
Houston, 2015). Spatial variations of tidal sensitivity for each type of tremors are estimated. Nankai and Cascadia subduction
zones have both ETS tremors and inter-ETS tremors, while tremors in Mexican subduction zone do not show significant alongstrike migration, and all tremors are categorized into inter-ETS tremors.
As for tremors in ETS, early tremor and later tremor show high sensitivity in Nankai subduction zone, while front tremor doesnot. In Cascadia, only after tremor does show tidal sensitivity. The absence of tidal sensitivity in early tremor in Cascadia isconsidered to be due to the smaller amplitude of tidal stress and/or stronger coupling of slow earthquake region. In the front
period, stress perturbation due to SSE slip would be larger than tidal stress, and tidal sensitivity disappears. After the SSE front
passes, plate interface get weakened, and strong tidal sensitivity will appear. Comparing with the amplitude of tremors estimatedby Yabe and Ide (2014), tidal sensitivity tends to increase from early tremors to later tremors where the amplitude of front tremors
is large. Because the amplitude of tremors is proportional to moment rate (Ide and Yabe, 2014), this observation is consistent
with the interpretation presented above. Tidal sensitivity also tends to be higher in shorter duration tremors, which is defined as
the half value width of tremor envelope. Considering the tremor model by Ando et al. (2010, 2012) and Nakata et al. (2011),
shorter duration might imply smaller tremor patch, which would not endure higher strain accumulation than larger tremor patch,
resulting in higher tidal sensitivity.

Keywords: Tectonic Tremor, Slow Earthquake, Subduction Zone, Tidal Sensitivity, Rate and State Friction Law

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SCG62-10

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Time:May 27 16:45-17:00

An estimate of fluctuating plate subduction velocities caused by tidal modulations anddecadal variations in the ocean
TANAKA, Yoshiyuki1∗ ; YABE, Suguru2 ; KIKUCHI, Ryosuke2 ; IDE, Satoshi2
1

ERI, Univ. Tokyo, 2 Department of Earth and Planetary Science, Univ. Tokyo

Non-volcanic tremors and slow slip events have been detected in plate subduction zones. The source areas of these events are
distributed in the transition zone located below the seismogenic zone, where high-pressure fluids supplied from the dehydrationof the subducted slab are decreasing the effective normal stress. Consequently, extremely small external stress disturbances cantrigger such events. Actually, variations in the tremor rate synchronized with diurnal and semi-diurnal tides have been observed.
In our previous study, a model to predict long-term variations in the tremor rate was constructed by considering modulations ofdiurnal and semi-diurnal tidal amplitudes in decadal time scales. Tremors and slow slips arise from slips on a plate boundary,so long-term variations in the occurrences of these events generate a fluctuation of a plate subduction velocity. By applying themodel to the Nankai area in Japan, it was found that the calculated tremor rate well corresponded to the long-term seismicity.
However, in their model, tidal and non-tidal ocean effects were not separated because observed tidal levels were used. Some paststudies estimated such non-tidal climatic effects on the seismogenic zone and concluded that the stress changes were insufficient
to trigger earthquakes. However, if considering the high sensitivity of the transition zone, smaller stress changes can fluctuate
a subduction velocity, which may eventually trigger earthquakes. In this study, employing an ocean model developed by theJapan Meteorological Agency, the effects of non-tidal ocean variations on such a fluctuation of slip rate are estimated for the
first time. The result indicates that the non-tidal effects are larger than the tidal effects in some regions. The fluctuation of slip
rate computed for a frictional parameter determined by observations of tremors exceeds 1 mm/yr at annual average in decadalscales, and periods with faster rates agree with some variations in seismicity. To quantitatively confirm if such slip variations are
sufficient to trigger large earthquakes, incorporating the stress disturbances into numerical simulations of earthquake cycles isnecessary.
Keywords: tides, slow slip, tremors, earthquake, seismicity, subduction zone

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SCG62-11

Room:303

Time:May 27 17:00-17:15

Tremor activity and slip modes controlled by the permeability of the megathrust boundary
NAKAJIMA, Junichi1∗ ; HASEGAWA, Akira1
1

Graduate School of Sci. Tohoku Univ.

Tremor activity in southwest Japan shows a sharp variation along the strike, but factors controlling such variation remain
largely unknown. We carry out seismic tomography using a large number of arrival time data to characterize seismic properties
around tremor activity, and find a close link between tremor activity and seismic properties above the plate interface. Tremor
is active underneath the moderate- to high-velocity overlying plate, while it is absent in areas overlain by distinct low-velocity
materials. High permeability along the plate interface enhances metamorphism of the overlying plate and prevents pore-fluidpressures from reaching near-lithostatic values. As a result, the plate interface is somewhat strengthened and slow slip no longer
occurs at short intervals. Our hypothesis explains the occurrence of long-term slow slip, instead of short-term slow slip, along
the inferred high-permeable plate interface in the Kii channel and eastern Kyushu.
Keywords: permeability, Philippine Sea plate

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SCG62-12

Room:303

Time:May 27 17:15-17:30

Seismic explosion survey on the episodic tremor and slow slip area in western Shikoku
TAKEDA, Tetsuya1∗ ; SHIOMI, Katsuhiko1 ; UENO, Tomotake1
1

NIED, Japan

Recently the Japanese Cabinet Office proposed the source model that would generate an anticipated maximum size mega-thrustearthquake along the Nankai trough. The down-dip limit of this model was based on the source regions of slow earthquakes
occurring along the subducting Philippine Sea plate. However, the relationship between the mega-thrust earthquake and slow
earthquakes has not been clear yet. Since the generation of slow earthquakes is strongly related to dehydration, there might besome characteristic structure around the source region of slow earthquakes.
To delineate the spatial geometry between slow earthquakes and plate boundary, and to investigate the structural variation along
the plate boundary, we conducted a seismic explosion survey in western Shikoku. The seismic line was aligned in the directionof NNW-SSE, passed through above one of dominant tremor clusters. We deployed 180 temporary stations with spacing of 450
m along the line. 300 kg dynamite was exploded as one shot on the midnight of 11th Dec, 2014.
We obtained good quality seismograms including many later phases. Two distinct phases with large amplitudes are identified
around 11-12 sec and 14 sec in two-way travel time, respectively. The former phase is expected to be reflections from the plateboundary in comparison to previous studies. The reflection would come from around the area where high pressure fluid would
exist, which was suggested by Shelly et al. (2006). We have a plan to work on the analysis to understand the accurate locationand the physical property variation of the plate boundary.
Acknowledgements: We thank the local governments along out survey line for cooperating our survey. The part of this study
is sponsored by ”Research project for earthquake disaster mitigation along the Nankai trough”.
Keywords: Seismic survey, Nankai trough, Plate boundary

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SCG62-13

Room:303

Time:May 28 09:15-09:30

Recurrence interval modulation of slow slip events by two types of earthquake loading
MITSUI, Yuta1∗
1

Institute of Geosciences, Shizuoka University

Geodetic studies have discovered recurrent spontaneous slow slip events (SSEs) at major faults. The SSE recurrence intervals
should reflect mechanical states at the faults, including load effects of large earthquakes in neighboring areas. Here, we focus on
temporal changes of the SSE recurrence intervals. We perform numerical model experiments with the rate- and state-dependent
friction to simulate the SSE recurrence interval changes by the earthquake loading effects. One result is gradual shortening of
the SSE recurrence intervals owing to nucleation process of nearby earthquakes, as revealed by several previous studies. Whenthe distance between the SSE and earthquake areas is almost zero, a short-term further decrease of the SSE recurrence intervals
precedes the earthquake occurrence (∼ by a decade). The other result is that external stress perturbation, as large as 0.1 MPa, canreduce the SSE recurrence intervals to a similar extent. Furthermore, the interval modulation by the stress perturbation continues
for a prolonged period until the occurrence of the adjacent earthquake. Both effects may be observable, as is advancing at the
Boso zone, Japan, but their separation is difficult under the present circumstances.
Keywords: Slow slip events, Stress perturbation, Rate- and state-dependent friction law, Earthquake preparatory process

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SCG62-14

Room:303

Time:May 28 09:30-09:45

Frictional properties of materials along the plate boundary of Tohoku subduction zone:
implications for slow slip events
SAWAI, Michiyo1∗ ; NIEMEIJER, Andre2 ; HIROSE, Takehiro3 ; PLUMPER, Oliver2 ; SPIERS, Christopher2
1

Hiroshima University, 2 Utrecht University, 3 Kochi / JAMSTEC

Episodic tremor and slip occurred just before the 2011 Tohoku-oki earthquake on a shallow portion (less than 20 km depth)in the Tohoku subduction zone (Ito et al., 2013). The area where slow slip occurred overlapped with the seismogenic zone.
To understand such diverse slip behaviour around the Japan Trench, not only the major earthquakes but also the slow slip
events, it is essential to reveal the frictional properties of rocks distributed at the Tohoku subduction zone. We thus conducted
friction experiments using a rotary shear apparatus on powders of blueschist (probably distributed at hypocenters at major Tohoku
earthquakes) and smectite-rich pelagic sediments (distributed along the shallow portion of the Tohoku plate boundary (Chester.,
et al 2013)). Simulated gouges were sheared at temperatures of 20-400o C, and effective normal stresses of 25-200 MPa and pore
fluid pressures of 25-200 MPa. We conducted velocity-stepping sequences (0.1 to 100 micron/s) to determine the rate and stateparameter (a-b) and investigated the effects of temperature, effective pressure and slip rate on slip stability.
Blueschist gouges show a friction coefficient of about 0.75 and positive (a-b) values which decrease to become negative withincreasing temperature. At 200oC, the behavior is velocity weakening and shows negative (a-b) values with a background frictionof ˜0.75. At 300oC, friction is ˜0.65 and the gouges show neutral to positive values of (a-b), showing larger (a-b) values thanat 200 oC. (a-b) values slightly decrease at 400oC with a background friction of ˜0.7. There is also effective normal stressdependence: even at temperature conditions where (a-b) tends to be positive, (a-b) values are negative at low effective pressure
and increase to positive with increasing effective normal stress. This suggests that increasing pore pressure is a possible factor
causing unstable slip, leading to slow slip events.
Smectite-rich pelagic sediments show that at low temperatures of 20 and 50oC, the simulated gouges exhibit negative values of(a-b) with a background friction coefficient of 0.38, except at the highest slip rate of 0.1 mm/s. However, the gouges show neutral
to positive values of (a-b) at temperatures of >100oC with the same background friction coefficient as at lower temperatures.
In addition, the value of parameter (a-b) depends significantly on slip rates: at temperatures of 20 and 50o C it increases fromnegative to neutral (or slightly positive at 20o C) with increasing slip rates to 0.1 mm/s, whereas it tends to decrease with increasing
slip rate at temperatures higher than 100o C. The downdip temperature limit of the slow slip events at Japan Trench (Ito et al.,2013) seems to be in the range between 100 to 150o C. The transition in (a-b) value from neutral to positive, particularly at lower
slip rates, occurs at the same temperature range. Hence, this could correspond to the observed downdip limit of the slow slip
events.

1/1

SCG62-15

Room:303

Time:May 28 09:45-10:00

Precise observation of migration of non-volcanic low frequency tremors by using dense
seismic array
TAKEDA, Naoto1∗ ; IMANISHI, Kazutoshi1 ; UCHIDE, Takahiko1 ; MATSUMOTO, Norio1
1

GSJ, AIST

Non-volcanic low frequency tremors (NVTs) in several major plate boundaries migrate with wide velocity range from 10 km/d
to over 50 km/h. The NVTs migrations are characterized by the velocity and direction. The fastest NVTs migration of thevelocity over 50 km/h is in either updip or downdip direction parallel to the slip direction of subducting plates [e.g. Ghosh et al.,G3, 2010; Ide, JGR, 2012]. Since March 2011, Geological Survey of Japan, AIST, performed the observation by a dense seismicarray in Mie prefecture. In this area, the active NVTs occur at intervals from 3 months to 6 months. Then, the seismic arrayrecords of over 10 times of major NVTs events were obtained to date. In this presentation, we located NVTs hypocenters by ananalyzing procedure same to the method of Ghosh et al. [G3, 2010] using our dense seismic array.
A sensitivity of the NVTs detection by using the seismic array is higher than a conventional envelope cross-correlation method.
However, the detection capability decreases, when the NVTs occurs roundly, as same as the case of the envelope cross-correlation
method [Takeda et al., JpGU, 2014]. Furthermore, the location accuracy is influenced by a distance and a velocity structure
between the NVTs hypocenter and the array.
Our observation infers that all the fastest NVTs migration around the array (within 25 km of epicentral distance) is in thealmost same direction during these three and half years. The migration direction is almost parallel to the slip of the subducting
plate, while some of events migrate in different directions. Furthermore, in some case, the direction changed temporary in thesame event.
To confirm a relation between these differences of migration directions and the detailed location of NVTs is future work.
Keywords: non-volcanic low frequency tremor, seismic array, Kii Peninsula

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SCG62-16

Room:303

Time:May 28 10:00-10:15

Activities about non-volcanic tremor beneath the Yatsushiro fault zone
MIYAZAKI, Masahiro1∗ ; MATSUMOTO, Satoshi2 ; SHIMIZU, Hiroshi2
1Grad. Sch. Sci., Kyushu Univ., 2 SEVO, Kyushu Univ.

Non-volcanic tremor induced by dynamic stresses has been detected in the Hinagu fault zone (Chao and Obara, 2012, SSJ).
We notice that the tremor occurred at the deep extension of the fault zone (Miyazaki et al., 2015, submitted). In addition, fromthe velocity structure estimated by sismic tomography (Matsubara and Obara, 2011), there are low P-wave velocity zone at the
deep part of the source region and high P-wave velocity anomaly in the shallow seismogenic zone. Therefore, the resolution is
not sufficiently enough, the tremor occurred in the brittle-ductile transient zone.
Investigating the stationary activities of non-volcanic tremor is important to reveal the crustal deformation process in the fault
zone. We performed the matched filter analysis (Gibbons and Ringdal, 2006) and detected the events (Miyazaki et al., 2014, SSJ).
However, most detected events were difficult to distinguish between signals and noises. In this study, we test the detectability ofsmall-scaled template events in the continuous seismic records including ambient noises using the same way conducted by Shelly
et al. (2006). We confirm that the scaled template events comparable to ambient noise level are detectable with same magnitudeof summed correlation coefficients as threshold values. This implies that a non-volcanic tremor without a disturbance occurredat the deep extension of the Hinagu fault zone has very small magnitude.
Keywords: non-volcanic tremor, Yatsushiro, Hinagu, active fault

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SCG62-17

Room:303

Time:May 28 10:15-10:30

Temporal variation of crustal resistivity in western Shikoku revealed by continuous MT
observations
YAMASHITA, Futoshi1 ; HONKURA, Yoshimori1∗
1

NIED

Various kinds of slow earthquakes such as deep low frequency tremors (Obara, 2002, Science), deep very low frequency
earthquake (Ito et al ., 2007, Science), and slow/long-term slow slip event (Hirose et al ., 1999, GRL; Obara et al ., 2004, GRL)
are observed in western Shikoku, Japan. In the lower crust of this area, existence of a characteristic low-resistivity structure wasrevealed by Magneto-telluric (MT) survey (Yamashita and Obara, 2009, AGU fall meeting). Since the low-resistivity structure
would be derived from fluids dehydrated from the subducting Philippine Sea plate, continuous MT observations are being carriedout to investigate relationship between the fluids and the activity of the slow earthquakes in this region. Since we succeeded todetect significant changes in the crustal resistivity by conducting careful data analyses, here we report the results. The continuous
MT observations were carried out in two observational sites KBN and SGW in Ehime prefecture from September, 2008 to March,
2010. One MT observational system was moved from SGW to a new observational site IKT in April, 2010 and the observations
are now continuing. To obtain highly reliable result by mitigating effects of noises, we followed the analytical method of Honkura
et al . (2013, Nature Communications), in which we used only data whose coherency between electric and magnetic fields waslarger than a threshold. Using the data, we calculated daily averages of apparent resistivity and phase. We further calculated
moving average of them over 31 data points to reduce data scattering, which intrinsically arises in the MT method. Since
the apparent resistivity shows annual variation due to atmospheric temperature variations, we removed it by using atmospherictemperature data obtained in Kuma observational site of Meteorological Agency. Number of analyzed frequencies of the MTdata is nine between 0.00055-0.141 Hz. As a result of analysis, we successfully detected temporal variations which satisfy thefollowing three conditions: (1) The apparent resistivity and the phase vary with antiphase at the same time. (2) The variations of(1) are similarly seen over several frequencies. (3) Similar variations are seen in two observational sites at the same time. Fromthese results, we considered that the temporal variations of the apparent resistivity and the phase are originated from changes in
the crustal resistivity. We then made a one-dimensional resistivity structure model based on the two-dimensional model revealed
by Yamashita and Obara (2009), and compared an observational change with the simulated one by forward modeling. The resultshows that the resistivity change in the depth between 20 and 25 km can approximately produce the observational changes in theapparent resistivity and the phase. We will further simulate how structural change can produce the observed variation based on
the two-dimensional resistivity structure and also investigate the relationship between the observed resistivity variation and theactivity of the slow earthquakes.
Keywords: Crustal resistivity, Magneto-telluric method, Slow earthquake, Subduction zone

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SCG62-18

Room:303

Time:May 28 10:30-10:45

Seismic activity and velocity structure in the Hikurangi subduction zone offshore theNorth Island of New Zealand
HAIJIMA, Daisuke1 ; MOCHIZUKI, Kimihiro1∗ ; HENRYS, Stuart2 ; SHIOBARA, Hajime1 ; YAMADA, Tomoaki1 ;SHINOHARA, Masanao1 ; FRY, Bill2 ; BANNISTER, Stephen2
1

Earthquake Res. Inst., Univ. of Tokyo, 2 GNS Science

The Hikurangi Plateau which has anomalously thick (˜12 km) oceanic crust subducts under the Australian plate along the
Hikurangi subduction zone offshore the North Island, New Zealand. The plate interface is shallow and we can identify the structure of plate interface in detail on the seismic reflection sections obtained by seismic surveys in the region [e.g., Bell et al. 2010].
Some topogrphic features on the plate interface such as seamounts and high-amplitude reflectivity zones have been identified.
The onshore GPS network has been develped since 2000 in the North Island, and the mechanical coupling coefficient along theplate interface has been estimated along the Hikurangi subduction zone. In its northern part (north of -40 degrees), the couplingregion is narrow and the down-dip limit is shallow at about 10 km depth. Although almost all of the coupling region is under thesea, ocean bottom seismic observation had not been conducted. Therefore, seismicity and hypocenter distribution in detail has
not been well understood. SSEs (Slow slip events) have been observed along the down-dip limit of the coupling region. They
occur at much shallower depths than other subduction zones. Tremors and swarms accompanying these events were also reported[Kim et al., 2010; Delahaye et al., 2009].
Marine seismic observation was conducted for the first time offshore Gisborne to observe earthquakes and low-frequency
events accompanying SSEs. Four OBSs were deployed in April 2012 and recovered after a year-long observation. The northern
two instruments were a broadband type and the other southern two were equipped with 1Hz seismometers. Although the data
recorder of one of the broadband type OBSs recorded only intermittently, good data were obtained from the others. During
the observation period, two major seismic events occurred around the OBS array. One of the events is a large SSE around the
Hawke’s Bay to the south of the array from mid-February 2013. First, I extracted event waveforms by applying the STA/LTA
event-detection algorithm, and determined hypocenters using manually picked P- and S-wave arrival times. Waveforms of these
events were, then, used as templates, and more events were detected by employing a Matched-filter technique. Differential arrival times were calculated by taking cross-correlation of waveforms of paired events. I applied double-difference tomographic
analysis (TOMODD [Zhang and Thurber, 2003]) to both absolute and differential travel time data. Focal mechanisms werealso calculated using P-wave polarity data. As a result, I successfully detected a number of events that were not observed by
the onshore seismic network, and determined their hypocenters. Although few events occurred on the seamounts and HRZs
along the plate interface, hypocenters are concentrated on the margin of the HRZ. In velocity structure analysis, I could resolve
structure under the offshore region where previous studies using data from onshore stations could not have resolution. However,these velocity structure models are in good agreement in the region where both results have resolved. Quite a few earthquakes
accompanying SSEs were observed. Seismic swarms which accompanied the past SSEs in this region occurred in the areas ofstably high seismicity. Small coupling regions which are caused by irregular topography of the plate interface may exist in theseares.
Keywords: seismicity, slow slip, plate interface, structure

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SCG62-P01

Room:Convention Hall

Time:May 27 18:15-19:30

Detection of seismic anisotropy from low frequency earthquake
ISHISE, Motoko1∗ ; NISHIDA, Kiwamu1
1

Earthquake Research Institute, University of Tokyo

Recently, members of family of slow earthquakes have been detected in a subduction zone by densely deployed seismic
observation network. They occur at the plate interface, and the source regions of them delineate the rupture zone of a futuremega-thrust earthquake in the southwestern Japan. Non-volcanic tremor is the most active phenomena within the family of slow
earthquakes and has been found to correlate temporally and spatially with other slow earthquake (e.g., Rogers and Dragert, 2003).
Therefore, there have been many studies on mechanism of non-volcanic tremor since the detection of the phenomena (Obara,
2002). However, the mechanism of the tremor has not been fully elucidated, although a lot of studies suggest a relationshipbetween tremor and fluid rebated from the subducting slab. Thus, we examine the relationship between fluid and the behaviorof non-volcanic tremor on the basis of special and temporal variations in seismic anisotropy, which is strongly related to the
behavior of fluid.
In this study, we detected seismic anisotropy at the plate interface of the PHS slab from the isolated phase during non-volcanic
tremor episode, which are categorized as low frequency earthquakes by the JMA (Nishide et al., 2000). The phases are regarded as
S-wave and used by hypocenter determination. Therefore, in order to detect anisotropy, we utilized S-wave splitting method (e.g.,
Ando et al., 1983), in which seismic anisotropy is represented by polarization direction of fast S-wave (direction of anisotropy)
and delay time between two S-waves.
Preliminary result of S-wave splitting analyses showed that the directions of anisotropy are tend to be orientated in the EastWest trending direction and the delay times are 0.2-0.4 sec. In general, however, anisotropy obtained by S-wave splitting analysis
is strongly affected by anisotropy near the receiver. In fact, the obtained anisotropy in this study is consistent with crust anisotropy
in the study area. In order to rigorously discuss anisotropy around the source region, we have to remove the effect of the anisotropy
in the crust.

Keywords: low frequency earthquake, seismic anisotropy, fluid

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SCG62-P02

Room:Convention Hall

Time:May 27 18:15-19:30

Observation of the deep low-frequency earthquakes using deep borehole-seismographnetwork. Activity in Tokai area
SUZUKI, Sadaomi1∗ ; OKUBO, Makoto1 ; ISHII, Hiroshi1 ; ASAI, Yasuhiro1
1

TRIES

Tokai area is the eastern side of Southwest Japan subduction where great earthquakes and deep low-frequency earthquakes(LFEs) occur along the convergent plate boundary. Researching the LFEs, Tono Research Institute of Earthquake Science(TRIES) installed a seismic array with 10 stations in Toyota city, Tokai area. Geological Survey of Japan (AIST) also installeda seismic array of three borehole-type instruments with high-sensitive seismographs at three depths of 50m, 200m, and 600m in
Toyota city. We used seismic data of those two arrays and SMYH station of Hi-net array of National Research Institute of Earth
Science and Disaster Prevention (NIED) as 3D array data for investigating LFEs. We successfully detected not only S waves but
also very weak P waves of LFEs using the 3D array data and the semblance method. We understood that 3D array observation
was effective for researching LFEs. We, therefore, built the second 3D array in Tono region where located 30-40 km north fromthe source region of LFEs in Tokai area.
We applied the deep borehole-seismograph network and the high density network of seismic stations of TRIES in Tono region
to the second 3D array. We called it Tono Juji array. Tono Juji array was constituted by two borehole stations of 1000 m depth,
three borehole stations of 500 m depth and twelve shallow stations. Seismic wave data observed by acceleration seismographs
were converted velocity data. All of the seismic wave data were unified to sample rate of 100Hz and filtered through a 2 to 10
Hz band pass filter. We selected a LFE with the maximum magnitude (M=0.6) among the 209 events from the JMA earthquake
catalog and named it LFE108. The origin time of LFE108 was 2014/9/1, 15h26m40.77s. We found a slight signal of P wave of
LFE108 in vertical component of each station. And we also found a slightly clear signal of S wave in horizontal component ofeach station. We could not find large difference in clear or unclear of the signals between borehole stations and shallow stations.
It means that the cause of unclear LFE signals mainly depends on not ground noise but overlapping of P, S and Coda waves ofmany successive LFEs.
Acknowledgements: We thank to Japan Meteorological Agency (JMA) and National Research Institute for Earth Science andDisaster Prevention (NIED).

Keywords: deep low-frequency earthquakes, deep borehole-seismograph network, array observation, semblance analysis

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SCG62-P03

Room:Convention Hall

Time:May 27 18:15-19:30

Automatic detection of low-frequency earthquakes in Southwest Japan using matchedfilter technique
MORIWAKI, Ken1∗
1

Japan Meteorological Agency

The Japan Meteorological Agency (JMA) has distinguished a class of events marked as low-frequency earthquakes in the
JMA’s earthquake catalog since 1999 [Nishide et al.,2000]. LFEs have clear isolated S phase with dominant frequencies lower
than ordinary earthquakes. The JMA’s earthquake catalog has about 24,000 events of tectonic LFEs in the Nankai Trough underSouthwest Japan from September 1999 to July 2014. Recent studies [Shelly et al.,2007] insist that tremor in the Nankai Troughconsists of a swarm of LFEs that occur as shear faulting on the plate interface. It is thought that watching activity of LFEs isimportant for supposing the state of the plate interface. However, it is difficult to detect LFEs by STA/LTA ratio, because of thelack of impulsive phase arrivals, used to detect and locate hypocenters of ordinary earthquakes. Therefore, it takes time to locate
their hypocenters in same procedure for ordinary earthquakes.
So, a matched-filter technique was used to detect events of tectonic LFEs in Southwest Japan automatically with the use ofcontinuous three-component velocity seismograms at 75 stations. These stations belong to the integrated seismic network ofJapan. 1,263 events which are listed in JMA’s earthquake catalog are used as template events. In analysis, first 2-8 Hz bandpass
filter was applied to templates and continuous seismograms, and these decimated to 20 samples per second. Template is 4
seconds time windows 1.5 seconds before the calculated S phase arrival. Next, the time window of template is shifted aroundthe calculated S phase arrival in an increment of 0.05 second through coutinuous seismograms.At each time point, correlation
coefficient value between templates and a part of continuous seismograms are computed , and the sum of correlation coefficientvalue for all stations is calculated. An event of LFEs can be detected when the sum of correlation coefficient value exceed athreshold. Finally, grid search method is used to make a hypocenter of detected event more precise. As a result of analysis, more
events listed in the JMA’s earthquake catalog have been detected after July 2014.
Keywords: low-frequency earthquakes, matched-filter technique

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SCG62-P04

Room:Convention Hall

Time:May 27 18:15-19:30

Spatial inhomogeneity of deep low-frequency tremor activity evaluated from seismic radiation energy and duration
ANNOURA, Satoshi1∗ ; OBARA, Kazushige1 ; MAEDA, Takuto1
1

Earthquake Research Institute, the University of Tokyo

Deep low-frequency tremor occurs associated with deep very low-frequency earthquake (VLF) and short-term slow slip event(SSE) on the interface of subducting Philippine Sea plate in southwestern Japan. Because they occur at the downdip part of themegathrust seismogenic zone, they are expected to be related to megathrust earthquake. Spatio-temporal distribution of tremor
has been well investigated to get a whole picture of tremor activity. However, during very active tremor period, envelope correlation between stations becomes relatively poor because of complicated waveforms. Then, it is difficult to detect and locate tremor
source during such active periods. On the other hand, radiation energy evaluated by squared velocity amplitude can be estimatedrobustly even if each waveform is complicated.
In this study, we developed a new tremor detection method with estimation of seismic radiation energy and centroid location.
This method extracts at first tremor sequence defined as a continuous tremor activity with amplitude exceeding a threshold.
Therefore, miss-detections of active tremor were reduced and it leads to more qualitative estimation of tremor activity. Thismethod was applied to tremor data in the Nankai subduction zone in 10.5 years starting from 2004.
From spatial distribution of seismic radiation energy by tremor, we found that very large tremor energy is radiated from western Shikoku area compared to that of previous studies. Spatial distribution of total duration and energy rate of tremor shows that
tremor zone can be classified into two types. One is an area which has high energy rate and long total duration such as westernpart of Shikoku or western part of Tokai. Another is an area which has low energy rate and short total duration such as central
western part of Shikoku or central part of Kii. On the other hand, a region of western Shikoku area has low energy rate but haslong total duration. Therefore, this part cannot be classified into two types. Comparison between distribution of tremor activity
and epicenters of large VLF suggests that most of VLF epicenters were distributed on the area which has high energy rate andlong total duration.
High energy rate indicates that the size of tremor is large. Therefore, tremor zone can be classified into area characterized bylarge size of tremor with long period or area characterized by small size of tremor with short period. On the other hand, a part ofwestern Shikoku is characterized by small size of tremor with long duration. This suggests that the size and duration of tremor
are independent each other and the tremor activity indicates spatial inhomogeneity.

Keywords: tremor, energy rate, duration

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SCG62-P05

Room:Convention Hall

Time:May 27 18:15-19:30

2014 Bungo channel slow slip event inferred from deep low-frequency tremor activity
OBARA, Kazushige1∗ ; TAKAGI, Ryota1 ; MAEDA, Takuto1 ; MATSUZAWA, Takanori2 ; TANAKA, Sachiko2 ;HIROSE, Hitoshi3
1

ERI, UTokyo, 2 NIED, 3 Kobe Univ.

Episodic tremor and slip is a stick-slip phenomenon in the transition zone between locked and stable sliding zones on theplate interface in Southwest Japan. The tremor burst with duration of several days spontaneously occurs at interval of several
months in each segment. On the other hand, in the Bungo channel region, the long-term slow slip event (SSE) occurs at every
6˜7 years at the updip side from the tremor zone. During the long-term SSE, continuous tremor activity was observed for a few
months in 2003 and 2010 at the updip part of the tremor zone which is neighbor to the source area of the long-term SSE. We
expected the next long-term SSE in 2016; however, tiny long-term SSE was inferred from tremor activity in early 2014, then
The Geospatial Information Authority of Japan reported the occurrence of the SSE (GSI, 2014). In this paper, we discuss therelationship between Bungo channel long-term SSE and triggered tremor.
Tremor activity seems to be quite different at its updip and downdip parts in the Bungo channel region. Tremor activity at the
updip part is well correlated with the crustal displacement caused by the long-term SSE; however, tremor activity at the downdip
part is constant with time irrespective to the occurrence of the long-term SSEs. The rate of the tremor number density which isthe number of tremor per 1 km square is nearly the same in both parts except during the long-term SSE. This indicates that thestandard rate of the tremor number density is independent from the depth. Because the triggered tremor by the long-term SSE
is added on the standard tremor rate at only the updip part, anomalous increase of the updip tremor may indicate a proxy for
SSE. Tremor activity at the updip part of the tremor zone in the Bungo channel seems to increase a little bit from the beginningof 2014. Then, small change in the crustal deformation was recognized from the middle of 2014 at southwestern Shikoku byusing GSI GEONET GNSS data. Similar small change in both tremor and GNSS data had been observed in the late 2006 and the
beginning of 2009. The 2006 small episode lasted for a few months. This is interpreted as the occurrence of very small long-term
SSE. On the other hand, the 2009 small episode was identified by tiny increase of tremor activity, then gradually appeared in
GNSS data, and finally evolved to the long-term SSE associated with significant slip and tremor activity from the beginning of2010. According to these previous examples, we expect that the small change observed by tremor and GNSS data in 2014 might
have stopped or will evolve to a regular long-term SSE before long.
After SSEs in 2003 and 2010, tremor activity seems to slightly increase in the inland region within 50 km from the triggered
tremor region in the Bungo channel. Such 7-year period variation in tremor activity is observed at only the updip side of thetremor zone. Moreover, pattern of the long-term variation seems to slightly migrate from the Bungo channel to east during a
few years. We might interpret that a tiny transient slip after the long-term SSE slowly propagates between the tremor zone andmegathrust seismogenic zone.
Keywords: non-volcanic tremor, slow slip event, slow earthquake, interaction, subduction zone

1/1

SCG62-P06

Room:Convention Hall

Time:May 27 18:15-19:30

Long-term ocean bottom monitoring for slow earthquakes on the shallow plate interface
in the Hyuga-nada region
YAMASHITA, Yusuke1∗ ; SHINOHARA, Masanao1 ; YAMADA, Tomoaki1 ; NAKAHIGASHI, Kazuo2 ;SHIOBARA, Hajime1 ; MOCHIZUKI, Kimihiro1 ; MAEDA, Takuto1 ; OBARA, Kazushige1
1Earthquake Research Institute, the University of Tokyo, 2 Graduate School of Science, Kobe University

The Hyuga-nada region, nearby the western end of the Nankai trough in Japan, is one of the most active areas of shallow slow
earthquakes in the world. Recently, ocean-bottom observation of offshore seismicity near the trench have succeeded to detectshallow tremor as a complete episode lasting for one month exhibiting similar migration property of deep tremor for the first time
[Yamashita et al ., in revision]. This activity was also associated with shallow very-low-frequency earthquake (VLFE) activity
documented by land-based broadband seismic network. The coincidence between tremor and VLFE and their migration patternshow strong resemblance with deep tremors during ETS episodes; this similarity suggests that the tremor activity in the shallow
plate boundary may also be coupled with VLF and short-term slow slip events (SSEs) in this area. However, the shallow SSEs
have not been detected to date, probably due to the lack of dense broadband seismic and/or geodetic observations in offshore. To
clarify the relationship among these slow earthquakes is important to improve the assessments of the potential of tsunamigenic
megathrust earthquake that is anticipated to occur at the Nankai Trough. Motivated by these issues, we started long-term oceanbottom monitoring in this area from May 2014 using 3 broadband and 7 short-period seismometers. To detect the suspectedshallow SSE, pressure gauges are mounted on the broadband ocean bottom seismometers for covering geodetic period range. In
January 2015, we replaced the instruments and obtained the first data which includes minor shallow tremor and VLFE activity on
June 1-3, 2014. Preliminary results of data analysis show that the shallow tremor activity occurred at the same area of the 2013activity, but clear tremor migration has not been found yet. However, it is promising to detect the large short-term SSE with ourdense and long-term observation including with pressure gauges in near future.
Keywords: shallow slow earthquake, Hyuga-nada, long-term ocean bottom monitoring

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SCG62-P07

Room:Convention Hall

Time:May 27 18:15-19:30

Very low frequency earthquakes in the shallow Nankai accretionary prism, following the2011 Tohoku-Oki earthquake
TO, Akiko1∗ ; OBANA, Koichiro1 ; SUGIOKA, Hiroko1 ; ARAKI, Eiichiro1 ; TAKAHASHI, Narumi1 ;FUKAO, Yoshio1
1

Japan Agency for Marine-Earth Science and Technology

A large number of shallow low frequency events were recorded after the 2011 Mw 9.0 Tohoku-oki earthquake by the cabled
network of broadband ocean bottom seismometers (DONET) deployed in the eastern part of the Nankai trough. This low
frequency event activity was intense for the first few days after the great earthquake and gradually decreased. Signals of theevents are most clearly visible at the frequency range around 2-8 Hz. Some of the events are accompanied by a very longfrequency (VLF) signal, which is clearly observed at around 0.02-0.05 Hz. The magnitude and source duration estimated by
waveform analysis for one of the largest very low frequency earthquakes (VLFEs) was 3.0 ˜3.5 and 17 s. This source duration isextremely long compared to ordinary earthquakes of comparable magnitude. These newly detected VLFEs are likely to be normal
fault earthquakes located at shallow depths within the accretionary prism, in contrast to the previously reported VLFEs that wereexplained by a low angle thrusting along the decollement zone. On the other hand, the low frequency events with no clear VLF
signal were previously regarded as being low frequency tremors (LFTs). We show that events with and without the VLF signal
likely represent the same phenomenon, and the VLF signal is only observed when a large magnitude event occurs near the station.
The waveforms of VLFEs are characterized by the coexistence of long source duration and high-frequency radiation of signals,
and such features were previously explained by the co-occurrence of shear failure and hydrofractures under the influence of fluid
brought into the decollement zone. Our result indicates that the stress state and the mechanical environment, which promote theoccurrence of VLFEs, exist not only along the decollement zone but also in the shallower part of the accretionary prism.
Keywords: Low frequency tremor, Very low frequency earthquake, Nankai trough, accretionary prism

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SCG62-P08

Room:Convention Hall

Time:May 27 18:15-19:30

Low frequency earthquakes associated with a very low frequency earthquake in southern
Ryukyu arc
TAKAHASHI, Tsutomu1∗ ; ISHIHARA, Yasushi1 ; MIURA, Seiichi1 ; KODAIRA, Shuichi1 ; KANEDA, Yoshiyuki2
1

JAMSTEC, 2 Nagoya University

Southern Ryukyu arc is an island arc located at southeastern part of Eurasian Plate. Recent seismic and geodetic studies
reported very low frequency (VLF) earthquakes near the Ryukyu trench (Ando et al. 2012) and slow-slip events beneath theislands in the southern Ryukyu arc (Heki and Kataoka, 2008). We have conducted seismic observation with 6 onshore stations
and 30 ocean bottom seismograms (OBSs) to elucidate seismicity, lithospheric structure and seismic events associated with VLF
earthquakes, as a part of ”Research project for compound disaster mitigation on the great earthquakes and tsunamis around the
Nankai trough region” funded by the Ministry of Education, Culture, Sports, Science, and Technology, Japan. Onshore stations
are deployed at Miyako-jima, Tarama-jima, Ishigaki-jima, Iriomote-jima, Kuroshima, and Hateruma-jima islands. They arecomposed of broadband (STS-2) and/or short period (1Hz) seismometers. OBS equipped with 4.5Hz three component geophone
were deployed around the onshore stations. When a VLF occurred at the southern Ryukyu arc during this observation, twodifferent low-frequency events (events-A and B) are observed by several OBSs. Events-A were observed only at the beginningof the VLF event. They recurred at intervals of 100 - 120 sec for about 20 min. Predominant frequency of these events areless than 5Hz, and duration times of oscillation are about 60 sec. Events-B recurred for about 3 hours, and most of theirduration times are longer than 100 sec. Predominant frequency is around 2˜3Hz, and the amplitude at high frequency (>5Hz)
are smaller than events-A. Spatial variations of amplitudes suggests that epicenters of Events-B would be located at north of
Events-A. Hypocenters of Events-A were estimated by P- and S-wave arrival times of OBSs. The hypocenters were relocated at
the southern end of the forearc basin, and their focal depths are about 15-20km. According to the seismic surveys in this area
(Hsu et al. 2013; Arai et al. 2015, JpGU), these hypocenters are located near the plate boundary. In future, we will conduct
envelope analysis with consideration of amplitude variation to clarify the detailed hypocenter locations.
Keywords: Low frequency earthquake, Ryukyu arc

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SCG62-P09

Room:Convention Hall

Time:May 27 18:15-19:30

Development on a method for automatically detection and location of very low frequency
earthquakes in JapanASANO, Youichi1∗
1

NIED

We have examined results of automatic detection and location of very low frequency earthquakes (VLFEs) in Ryukyu, southern
Japan. In this system, three component seismograms recorded at the NIED F-net were analyzed by using waveform-correlation
and back-projection techniques after processing a band-pass filter (0.02 to 0.05 Hz). Here we used known 6 VLFEs and 17
regular interplate earthquakes near the trench axis as template events. Time series of cross-correlation function (CC) at eachstation was calculated from continuous waveform data and triggered seismograms of template events. Assuming surface wave
propagation, CCs are back-propagated onto possible origin times and horizontal locations. We obtained epicenters of VLFE
candidates by performing a grid search in time and space domains to maximize the averaged CCs from all stations under thecondition of high signal to noise ratios that was defined as amplitude ratios between two time windows before and after thesurface wave arrivals from the VLFE candidates. We applied this method to the F-net data on November 29, 2014, when VLFEs
occurred in Ryukyu, where only six stations are available for the analysis. Small number of stations easily causes errors in our
detection and location of VLFEs probably due to aliasing in space domain. As the results of analysis, most of the VLFEs weredetected and located off Ishigakijima Island. These epicenter locations are consistent with surface wave arrival from the VLFE
candidates. However, some events were located between Okinawa Island and Miyakojima Island. This suggests that the present
method needs additional development considering arrival times.
Keywords: very low frequency earthquake, automatic detection, automatic location

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SCG62-P10

Room:Convention Hall

Time:May 27 18:15-19:30

Detection and mechanism determination of VLF earthquakes in the Guerrero subduction
zone
MAURY, Julie1∗ ; IDE, Satoshi1
1Grad. Sch. Sci., Univ. Tokyo

Very Low Frequency (VLF) earthquakes have been observed with tremors in a few subduction zones suggesting a common
source for the two phenomena. However to investigate more precisely the relation between these phenomena, VLF signal should
be looked for in other subduction zones where tectonic tremor occurs. The Guerrero subduction zone is such an area where
tremors have been consistently detected. Following the method of Ide and Yabe [2014], by stacking signals in the VLF band
between 0.02-0.05 Hz at the time of occurrence of tremors, we confirm that VLF earthquakes are also observed.
MASE experiment data from 2005 to 2007 are used to determine the location of tremors and VLF earthquakes. They are foundin two places tremors are detected, the southern transient cluster and the northern, more persistent, cluster. Both are locatednear the flat part of the subduction interface. This seems to confirm that VLF earthquakes are produced by shear failure near
this interface. The VLF signals are then inverted to estimate the moment tensor of these events. Due to the linear geometryof the MASE experiment the mechanism is not well constrained but one of the nodal plane is generally nearly horizontal inaccordance with the distinctive geometry of the subduction and the slip direction is globally coherent with the convergence
direction. Moreover, the plunge of the P and T axis are well constrained with values of about 40 ⁰ adding a constraint on theprincipal stress directions.

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SCG62-P11

Room:Convention Hall

Time:May 27 18:15-19:30

Broadband source spectrum of a slow slip event in the Cascadia subduction zone
TAKEO, Akiko1∗ ; HOUSTON, Heidi2 ; CREAGER, Kenneth2
1

Hokkaido University, 2 University of Washington

Slow earthquakes have been discovered in various time scales: non-volcanic tremor at high frequency range of 1-10 Hz, very
low frequency earthquake (VLFE) at intermediate range of 10-100 s, and slow slip event (SSE) at geodetic time-scale longer than
one day. Since these phenomena occur simultaneously, tremor and VLFEs can be regarded as the high frequency componentsof SSE. Based on this idea and to discuss the source time function of a SSE for the first time, we estimated source spectrumof Mw 6.8 episodic tremor and slip (ETS) event in the Cascadia subduction zone in 2010 from tremor band to the VLFE band.
The source spectrum in the tremor band can be simply obtained by correcting the effect of attenuation and geometric spreading.
The source spectrum in the VLFE band is more complicated because the signal-to-noise ratio is about one. We first improved
the signal-to-noise ratio by stacking waveforms at a period range of 20-50 s with an assumption that the VLFEs coincide withpeaks of tremor amplitudes. We then obtained source spectrum at 30-100 s by dividing the spectrum of stacked waveforms by thespectrum of synthetic waveforms corresponding to the obtained focal mechanism. The obtained source spectrum is proportional
to inverse of frequency in both tremor and VLFE bands. In addition, the spectrum in both bands could be roughly fit by asynthetic source spectrum corresponding to a boxcar shaped source time function whose duration is about ten hours and the total
moment release is Mw 6.8. The apparent duration of ten hours is shorter than the observed duration of the ETS, one month. This
result indicates that the moment release during the one-month ETS consisted of slip pulses with typical durations shorter than aday.
Keywords: very low frequency earthquake, tremor, slow slip event, Cascadia

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SCG62-P12

Room:Convention Hall

Time:May 27 18:15-19:30

Basic study on detecting short-term SSE by using GPS and tiltmeter data
AOKI, Natsumi1∗ ; KUZUHA, Yasuhisa2 ; KIMURA, Takeshi3
1

Faculty of Bioresorces, Mie University, 2 Graduate School of Bioresorces, Mie University, 3 National Research Institute for Earth
Science and Disaster Prevention
We tried to detect short-term slow slip event by using both GPS and tiltmeter data. Detecting procedure for GPS-detecting isalmost Nishimura’s and titlmeter-detecting is similar to that of Kimura et al. However, we focus on spatial distribution of SSE.
Takeshi Kimura, Kazushige Obara, Hisanori Kimura and Hitoshi Hirose, Automated detection of slow slip events within the
Nankai subduction zone, GEOPHYSICAL RESEARCH LETTERS, VOL.38, L01311, doi:10.1029/2010GL045899, 2011.
Takuya Nishimura, Takanori Matsuzawa, and Kazushige Obara, Detection of short-term slow slip events along the Nankai
Trough, southwest Japan, using GNSS data, JOURNAL OF GEOPHISICAL RESEARCH: SOLID EARTH, VOL.118, 31123125, doi:10.1002/jgrb.50222, 2013.

Keywords: SSE, GPS, Tiltmeter, AIC

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SCG62-P13

Room:Convention Hall

Time:May 27 18:15-19:30

A test for detecting slow deformation around Japan based on seismicity data and statistical
model
KATAOKA, Jun1 ; MITSUI, Yuta2∗
1

Faculty of Science, Shizuoka University, 2 Institute of Geosciences, Shizuoka University

Slow slips that occur at much slower slip rates than ordinary earthquake have been mainly detected by geodetic techniquessuch as GNSS. However, where there is no observation point in the vicinity of the source region or before dense GPS observation
began, it is difficult to detect slow slips by the geodetic techniques. In this study, therefore, we apply the ETAS model (a typeof statistical model) to the data of a seismic catalog, for detecting slow slips around Japan. Specifically, I focus on increaseof values of a parameter called background seismicity rate after removing the effects of aftershocks. Results of the parameter
estimation for known slow slip events showed that we can detect slow slips occurring over several days to weeks. Moreover, theresults suggested that slow slip events around the north Izu-Ogasawara Trench and Kikai Island occurred, and slow deformation
by a dike intrusion occurred around Mt. Fuji immediately after the 2011 Tohoku earthquake. In addition, around Okushiri island,
Kikai island, Tanegashima island, and off Tohoku area, we possibly detect seismic quiescence or temporal attenuation of afterslip
after large earthquakes.
Keywords: slow slip, ETAS model, earthquake activity, background seismicity rate

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SCG62-P14

Room:Convention Hall

Time:May 27 18:15-19:30

Estimation of frictional parameters on the SSE fault throuth Ensemble Kalman Filter
OKUDA, Ryosuke1∗ ; HIRAHARA, Kazuro1 ; MIYAZAKI, Shinichi1 ; KANO, Masayuki2 ; OHTANI, Makiko1
1

Graduate School of Science, Kyoto Univercity, 2 Earthquake Research Institute, University of Tokyo

Slow slip events (SSEs) occur repeatedly on the plate interface beneath the source regions of the interplate large earthquakes.
The activity of SSE possibly changes before the occurrence of large interplate earthquakes (Peng and Gomberg, 2010). Hence,
it is essential to know the frictional properties for producing SSEs to predict the occurrence of large earthquakes. Our final goal
is to optimize frictional parameters on the fault related to SSE with GPS data through Ensemble Kalman filter (EnKF), a data
assimilation method which combines the observational data and the forecast values derived from a simulation model, and then to
give some insight on the occurrence of large interplate earthquakes. In this paper, we construct the synthetic data from simulated
slip velocity on the observation error. Then, we perform numerical experiments on estimation of frictional parameters through
EnKF, verifying the estimated values and their errors.
In this paper, we focus on Yaeyama SSEs along the Ryukyu trench, southeast Japan. Around the Yaeyama islands, GPS observed southeast displacement related to SSEs recurrently. Heki and Kataoka (2008) reported the following features of Yaeyama
SSEs; 1) there are few earthquake near affecting the SSE fault in the observation period ,2) SSEs recur on a plate interface at
depths of 20-40km, 3) the average recurrence interval is 6.3 months, 4) its standard deviation is 1.2 months, 5) the slip rate
released by SSEs is 11.0 cm/yr, in spite of the estimated convergence rate of 12.5 cm/yr.
We construct a simulation model which reproduces the above features of SSEs. We set a dipping fault embedded in a homogeneous elastic half space. The friction on the fault is assumed to obey a rate-and state-dependent friction law, and the slowness lawof state evolution (Dietrich, 1979). We set an asperity at depths of 20-40 km on a stable sliding plate interface, whose frictional
properties are characterized by frictional parameters A, B and L following Kato (2003). The asperity has the velocity weakening
frictional property of A-B<0 and its radius is nearly equal to or less than the nucleation radius determined by frictional parameters. We successfully reproduce the SSEs with the recurrence interval of about 6 months by setting a single asperity with theradius of about 30 km has frictional parameters of Vpl=12.5cm/yr, A=50 kPa, B=57.5kPa, and L=2.5 mm.
We perform numerical experiments on estimation of frictional parameters on the fault through EnKF with the constructed
model. EnKF is the method for estimating optimum values by sequentially modifying the observations, simulated results andtheir variance-covariance matrix in a statistical way. The variance-covariance matrix are calculated by computing a lot of ensemble members which are generated by adding random numbers to initial values. As a first step, we generate the synthetic date as
observed values by adding random noise to slip rate on the fault simulated on the above physical model and frictional parameters.
Those parameters and calculated values are defined as true values on the experiments. We estimate slip rate, state variable andfrictional parameters, A, A-B, and L thorough EnKF with the synthetic data and initial parameters with added offsets to true
value, and verify the result by comparing the estimated values to true values.In this presentation, I show the verified result.
Keywords: slow slip events, Ensemble Kalman Filter

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SCG62-P15

Room:Convention Hall

Time:May 27 18:15-19:30

Modeling various slow slip events along the Hikurangi subduction zone
SHIBAZAKI, Bunichiro1∗ ; MATSUZAWA, Takanori2
1

International Institute of Seismology and Earthquake Engineering, Building Research Institute, 2 National Research Institute for
Earth Science and Disaster Prevention
Recent high-resolution seismic and geodetic observations have revealed the occurrence of slow slip events (SSEs) along various
subduction plate interfaces. Long-term SSEs with a duration of 1.5 years (e.g., Manawatu SSEs) occur at the deeper portion (25–
60 km) of the Hikurangi subduction zone, and shallow (5–15 km) SSEs with a duration of 1–3 weeks occur along the northernand central parts of the subduction zone. Wallace et al. (2012) reported a sequence of simultaneous short-term and long-term
SSEs at the Hikurangi subduction zone during 2010–2011.
We modeled short-term and long-term SSEs along the Hikurangi subduction zone using a rate- and state-dependent friction
law and considered realistic configurations of the plate interface. We set the coupling region where a-b is negative based on the
study of interseismic coupling by Wallace et al. (2009). By setting the effective stress and the critical displacement of shallow
short-term SSEs to approximately 1.5 MPa and 2.4 mm, respectively, we could reproduce SSEs with a duration of 1–3 weeks
and recurrence interval of 3 years. Additionally, by setting the effective stress and the critical displacement of the Manuatsu
long-term SSEs to approximately 3.0 MPa and 7.2 mm, respectively, we were able to reproduce SSEs with a duration of 0.5
years and recurrence interval of 5 years. The effective stress of the Manawatu SSE zone is two times larger than that of theshort-term SSE zones. However, the ratio of the effective stress to the critical displacement of the Manawatu SSE zone is smaller
than that of the short-term SSE zones. We could also reproduce a sequence of simultaneous short-term SSEs and a long-term
Manawatu SSE as observed by Wallace et al. (2009). The occurrence of the various slow slip events suggests heterogeneous
distributions of constitutive law parameters along the Hikurangi subduction zone.
Keywords: modeling, slow slip events, Hikurangi subduction zone, a rate- and state-dependetn friction law, shallow short-term
SSEs, Manuatsu long-term SSEs

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SCG62-P16

Room:Convention Hall

Time:May 27 18:15-19:30

Earthquake cycles on the bumpy plate interface assuming subducting ridge chain : generation of SSE
OHTANI, Makiko1∗ ; HIRAHARA, Kazuro1
1Sci., Kyoto University

Recently the seismic and the geodetic observation networks have observed the slip events on the plate interface in subduction
zones, in multiple scales in time and space. These slip events are densely distributed on the plate interface, and considered tointeract to each other. And then, their interactions with large earthquakes are now starting to be investigated, using ECSs (Earthquake Cycls Simulations) (Ariyoshi et al., 2014; Matsuzawa et al., 2013).
When we consider the actual large earthquakes, the fault system such as the topography of the plate interface plays an important role on the occurrence of the earthquakes. However, the previous studies consider only the relatively large scale of the
topography for the plate interface (e.g., Hirose and Maeda, 2013). In this study, we focus on the subducting ridge chains in Tokai
regions, as the fault topography in the smaller scale. The ridge chain subducts under the Tokai region, central Japan. We candetect them in the bathymetry data (Hirose and Maeda, 2013). From the survey of velocity structure, we can also observe theridges subduct with the oceanic plate (Kodaira et al., 2004). In the Tokai region, the next Tokai earthquake is anticipated to occur
in the first half of this century. In the deeper part of the Tokai region, there have been observed also long-term slow slip events(SSEs) just beneath the Lake Hamana (Tokai SSEs). In this study, we set the bumpy plate interface assuming subducting ridge
chain, and examined the slip cycles on the plate interface.
For ECSs, we often use the boundary integral elemental method and the quasi-dynamic scheme, which have smaller computational amount. Such ECSs always consider only the shear stress change but not the normal stress change due to the slip.
However, the normal stress changes due to the slip on the fault interface when the fault interface is not flat but has topography.
Therefore, in this study, we introduced the static normal stress change to the quasi-dynamic ECSs in BIEM, and examined theslip behaviors on the bumpy plate interface.
Now, as the fault, we set the flat plate interface of 200 km × 240 km for strike and dip directions, which subducts with thesteady subducting velocity of 3.25 cm/year and the subducting angle of 15 degrees. We also set the bumpy plate interface as
the fault, which has three bumps with the height of 5 km on the above flat plate interface. And then, we compare the earthquake cycles on the two plate interfaces to investigate the effect of the fault topography. We assume the laboratory derived rateand state-friction law with the normal stress change (Linker and Dieterich, 1992). We set the uniform initial shear and normal
stresses. The frictional parameters are set to be uniform at the region shallower than the depth of 40 km.
Then, even with the frictional condition that produces repeated normal earthquakes, the bumpy fault interface produced repeated slow slips and the earthquakes. A series of the tops and valleys of the ridges exhibit the increase and decrease in thenormal stress during the interseismic period. This striped normal stress change can be the cause for recurring slow slip events
around the valley of the ridge chain, because the change in the normal stress leads to the change in the friction. The Tokai SSEs
are observed at the valley of the ridges. This study shows that the fault geometry can be one of the mechanism of generating theTokai SSEs, in addition to the existence of high pore pressure.
Keywords: earthquake cycle simulation, normal stress, ridge chain, Tokai SSE

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SCG62-P17

Room:Convention Hall

Time:May 27 18:15-19:30

Simulation of slow earthquakes affected by tide
KURIHARA, Ryo1∗ ; ANDO, Ryosuke2 ; YABE, Suguru2 ; TANAKA, Yoshiyuki1 ; OBARA, Kazushige1
1Earthquake Research Institute, The University of Tokyo, 2 Graduate School of Science, University of Tokyo

Slow earthquakes occur at the deeper extension from the seismogenic zone along subducting plate interfaces and may affectoccurrence of large earthquakes. Therefore, it is important to understand the physical mechanism of slow earthquakes. On
the other hand, the tides are one of important factors that affect slow earthquakes and possibly large earthquakes suggested by
Tanaka[2012], who found increasing tidal sensitivity of seismicity toward a large earthquake.
In order to investigate quantitatively the influence of the tides on the recurrence process of earthquakes, we develop a physicalmodel of slow earthquakes with the tidal effects.
In the primary model, we considered a 2-D fault embedded in the elastic half-space, mimicking as a subduction plate boundary.
We divide the fault into the shallower coupling area and the deeper decoupling area. The coupling area has a frictional strengthobeying the slip weakening law, associated with the velocity strengthening term to simulate slow slip events. The decoupling area
obeys monotonic velocity strength, exhibiting steady slip by the tectonic loading and tidal stresses. We consider the following
two cases in the tidal stresses: the simplified sinusoidal function that has the constant amplitude and the period, and the realistic
case, in which we calculated the amplitude and the phases along the upper boundary of the subducting Philippine Sea plate inwestern Shikoku area. Both of the Earth and ocean tides are considered. The tectonic loading is assumed as the back slip model.
We employ quasi-dynamic boundary element method for the numerical simulations.
As the results, we found that the tides actually modulate the timing of the slow earthquake occurrence. The migration velocity
might also be modulated by tides. In addition, we confirmed that slow ”pre-slip” events occur in the small area at the bottom of
the coupling area before large slip events, and they are modulated by the tides. The tides also seem to control the stoppage of slip
events and further affect the distribution of the residual stress.

Keywords: slow earthquake, tide, source migration

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