SCG57-P01

Room:Convention Hall

Time:May 27 18:15-19:30

Dynamics that connects massive earthquake and cross section structure of Aomori, Iwate,
and Miyagi
MASE, Hirofumi1∗1none

In convergence zones, high temperature bodies are formed diagonally-on-and-under the plate of low temp. and the bodies are
drawn each other. The mantle wedge and the plate, get on the high temp. body that heads westward from the east, head westward.
And, they are placed by the high temp. body that heads eastward from the west and compressed. I think this is the main springand structure in it. I explained in each respect of the theory, experiment, and application.(1)(2)This time concerns the structural understanding of the north off Miyagi. First of all, I can recognize the feature of Miyagi(Sectiond-d’) again by the comparison with Aomori(Sec. a-a’). Hot4 of the high temp. is extended to the west more and Hot5 is extended
to the east more. And, the direction of the main spring is almost horizontally. Moreover, because there is no remarkable hot
section in (the wedge in the east coast east)(W), modeling and repro.-experiment in the slip zone of 3.11 were easy. Hot4 thatsurges from the west has the tendency to be stuck well to the slope in the east part, and stagnates. And, the material accumulates
about there. As a result, the land is formed and maintained. However, in the eastern edge, pressure tends to come off to the undereast. Because W is pushed from the west true side, flaking-off along the boundary can be expected.
The feature of Aomori is entirely different. Because Hot 4 and Hot 5 do not extend, the angle of the mainspring and the slope
is squarely near. And, Hot 4 approaches the slope first and develops along it. Therefore, the land does not develop. Because W
is pushed from the under west diagonally, flaking-off deviates from the boundary on the way and pushes up bottom of the sea.
Material collects there and Dome develops. Because, on the east side from that place, power to stop the Dome is generated in thereaction from the under east diagonally, flaking-off along the boundary will not happen easily here similarly. Though Sec. a-a’and Sec. b-b’ look like, more active slip of climbing up the slope is expected in the former because it has the engine(Hot 1) alsoin W. Region AO in the Plane chart is peculiar in these reasons.
In comparison with off Miyagi, following matters were mysterious (8). In the large earthquake(EQ) in 1968 and 1994, theposition of initial rupture(IR) and main rupture(MR) is mutually away (7). It seems the 1994 EQ destroyed from the shallow tothe depth widely (13).
However, according to the above-mentioned structural understanding, it can explain that the characteristic of large EQ in region AO is having the seismic source process that ,on the east side of the Dome, the stopper moves first(IR) and ,west side, thelarge slip starts(MR).
The temp. structure of Iwate(Sec. c-c’) is intermediate as a whole. It is peculiar that there are low temp. bodies under the land
and there is huge Hot 3 in W. Hot 3, Hot 4, and Hot 5 pull each other mutually. The underground is pushed from east and west
and the land is supported by steady pressure. I think that Sanriku can exist for this. Because Hot 3 is pulled to the under east
diagonally, point of W and subducting slab are pushed immediately. This and earthquake-prone zone(9) relate.
(1)MASE/SSJ2010/P3-47 (2)MASE/JpGU2012/SCG67-P06 (3)MASE/SSJ2012/P2-75 (4)MASE/JpGU2013/SSS28-P09 (7)NAGAI et al.(2000)/ERI U-Tokyo (8)MASE/JpGU2014/SSS30-P01 (9)JMA/Monthly Report/July 2005 (13)SendaiDMO,JMA/The
1994 Far Off Sanriku Earthquake

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SCG57-P02

Room:Convention Hall

Time:May 27 18:15-19:30

Crustal study of the Northern Scandinavian Mountains from receiver functions analysis
and surface wave ambient noise
BEN MANSOUR, Walid1∗ ; MAX, Moorkamp1 ; ANDREAS, Kohler2 ; STEWART, Fishwick1
1

University of Leicester, 2 University of Oslo

The Scandinavian Mountains are a topographic anomaly on the North-East Atlantic passive margin. With heights above 1
km adjacent to the low-lying Baltic Shield ( average altitude of 500 m), this mountain range has undergone a rejuvenation by
an uplift event during the Neogene. The absence of a crustal root expected from Airy isostasy calculations , the variation ofgravity anomaly and the possibility of a low velocity zone in the upper crust suggest variations in density within the crust. Thismechanism will explain the (isostatic) equilibrium of the mountain range. With this perspective two passive seismic experiments
were deployed in 2007-2009 (SCANLIPS2) and 2013-2014 (SCANLIPS3D) across the Northern Scandinavian Mountains. These
2 experiments allow a better characterization of the crust in terms of Moho depth, Poissons ratio and shear wave velocity. Herewe will show a new Moho map compiled from our new results together with previous studies (LAPNET-POLNET, SNSN andNORSAR network) in this region. This map shows a crustal thickening from West to East (40 km to 50 km) without any obvious
influence of the transition from the Scandinavian Mountains to the Baltic Shield. From our receiver functions only, inverse
modelling does not confirm the presence of a low velocity zone in the upper crust as suggested in previous work in the area
using P receiver functions and controlled source experiments. We therefore use Rayleigh waves ambient seismic noise to better
constrain the shear wave velocity at the short periods (3- 30 s). Finally a joint inversion of the P-receiver functions and surface
wave ambient noise used to build a new 2D crustal model across the Northern Scandinavian Mountains. This new crustal model
confirms the assumption of the variation densities within the crust like the source of this topographic anomaly on this passive
margin.
Keywords: Scandinavian Mountains, Neogene uplift, variation density, P-Receiver Functions, Rayleigh waves dispersion curve,
joint inversion

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SCG57-P03

Room:Convention Hall

Time:May 27 18:15-19:30

Seismic velocity structure off the Boso Peninsula, Central Japan, revealed by an ocean
bottom seismographic experiment
KONO, Akihiro1∗ ; SATO, Toshinori1 ; SHINOHARA, Masanao2 ; MOCHIZUKI, Kimihiro2 ; YAMADA, Tomoaki2 ;UEHIRA, Kenji3 ; SHINBO, Takashi3 ; MACHIDA, Yuya4 ; HINO, Ryota5 ; AZUMA, Ryosuke5
1
5

Graduate School of Science, Chiba University, 2 Earthquake Research Institute of Tokyo University, 3 NIED, 4 JAMSTEC,
Graduate School of Science, Tohoku University

Off the Boso Peninsula, central Japan, where the Sagami trough is in the south and the Japan trench is in the east, there is a
triple junction where the Pacific plate (PAC), the Philippine Sea plate (PHS) and the North America plate (NA) meet each other.
In this region, PAC subducts beneath PHS and NA, and PHS subducts beneath NA. Due to these subductions, numerous seismic
events took place in the past, such as the Enpo-Boso earthquake 1677, Genroku-Kanto earthquake 1703, the Taisyo-Kanto earthquake 1923, and the Boso slow slip events. In order to understand these events, it is important to image structure under Kanto
region, and many researchers attempted to reveal the substructure from natural earthquakes and seismic experiments.
Because most of the seismometers are placed inland area and the regular seismicity off Boso is inactive, it is difficult to reveal
the precise substructure off Boso area only from analyzing natural earthquakes. Although several marine seismic experiments
were held, vast area remains unclear off Boso Peninsula. In order to improve the situation, a marine seismic experiment was
conducted from 30th July until 4th of August,2009. The survey line has 216 km length and 20 Ocean Bottom Seismometers(OBSs) were placed on it.
In this study, we analyzed the airgun data acquired from the OBSs by using PMDM(Progressive Model Development Method;
Sato and Kenett, 2000) and FAST(First Arrival Seismic Tomography, ;Zelt and Barton, 1998), then obtained 2-D seismic velocity
structure.
According to the previous studies, the P wave velocity of the upper surface of Philippine Sea plate (UPHS) is around 5 km/s,
then, we drew the line which represents the UPHS at 5.0 km/s zone. The result shows that the UPHS inclines gently toward east,and the high P-wave velocity area which has 35 km width, locates off southernmost Boso Peninsula, 4 km depth from the sea
surface.
The estimated depth of UPHS corresponds to that of Nakahigashi et al.(2012) and Kimura et al. (2009). We also compared
our result with other studies and delineated the isodepth contours of UPHS off the Boso Peninsula. We gained a rough image
that the 10 km isodepth contour is almost parallel to the Sagami trough, the 15 km isodepth contour runs toward east, and the 20
km isodepth contour runs toward northeast. It indicates that the Philippine Sea plate subducts gently off the Boso Peninsula andit gets sharpened gradually toward the land.
The width and location of the high P-wave velocity area correspond to that of a bump on the UPHS revealed by Tsumura et al.
(2009). The velocity is higher than 6 km/s in the center therefore, we concluded that the bump is the buried seamount and our
result supports the result of Tsumura et al. (2009).
Acknowledgement
The marine seismic experiment was conducted by R/V Hakuhou-maru of Japan Agency for Marine-Earth Science and Technology, and the OBSs were retrieved by Shinchyo-maru of Shin-Nihon-Kaiji co. Ltd. (Present, Fukada salvage co. Ltd.).
We would like to thank captains and the crew of Hakuho-maru and Shinchyo-maru.
This study was supported by the Ministry of Education, Culture, Sports, Science and Technology (MEXT) of Japan, under its
Observation and Research Program for Prediction of Earthquakes and Volcanic Eruptions.

Keywords: Off-Boso, Seismic velocity structure, Philippine Sea plate

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SCG57-P04

Room:Convention Hall

Time:May 27 18:15-19:30

Compilation of thermochronologic ages of bedrocks in Japan: For understanding the deformation over geologic time
SUEOKA, Shigeru1∗ ; TAGAMI, Takahiro2
1

Japan Atomic Energy Agency, 2 Division of Earth and Planetary Sciences, Kyoto University

For understanding of the relationships between stress and strain and separation of elastic and inelastic deformations in the crustof the Japanese Islands, comparison and investigation of deformations over various time scales are significant (e.g., Ikeda et al.,2012; Nishimura, 2014). The authors are attempting to estimate vertical strain rate of the NE Japan Arc over geologic time byusing low-temperature thermochronology, as a part of “Crustal dynamics ― Unified understanding of intra-island deformation
after the great Tohoku-oki earthquake ― ” . Although vertical deformation in the NE Japan Arc over the geologic time has
been investigated in the plains and coastal areas on the basis of the relative heights and formation ages of the marine and fluvial
terraces (e.g., Koike & Machida, 2001; Tajikara & Ikeda, 2005; Matsu’ura et al., 2008, 2009), few quantitative data is available
in the mountainous regions where higher uplift rates are possible. As the preliminary step toward thermochronometric studies
in the mountainous regions in the NE Japan Arc, we compiled previous thermochronometric ages over the Japanese Islands toreview previous thermochronometric data in the NE Japan Arc and to understand vertical deformation of the Japanese Islands
over the Japanese Islands. We are compiling mainly about fission-track (FT) ages regarding the items, such as author(s) andyear of publication, journal, study area, lithology, sample code, latitude, longitude, altitude, apatite FT age and error, zircon
FT ages and error. At present, we have compiled >350 apatite FT ages and >600 zircon FT ages from >70 articles including
unpublished data. The result of the compilation suggests: 1) still more data have been reported in the SW Japan Arc than in the
NE Japan Arc, 2) in the Kitakami and Abukuma regions, pacific coasts of the NE Japan, apatite FT and zircon FT ages of late
Cretaceous were reported (Goto, 2001; Ohtani et al., 2004), indicating total denudation since that era is less than 2-3 km, and
3) in the Iide and Echigo mountains along the Japanese Sea coast of the NE Japan, a few apatite FT ages younger than the endof Neogene were obtained (Goto, 2001; Sueoka unpublished data), implying recent rapid uplift and denudation. By following
the compilation results, we are planning to apply thermochronometric methods, e.g., FT analyses and (U-Th)/He dating, to themountainous regions in the NE Japan Arc, especially in the areas where young ages were reported or no age was obtained.
Keywords: thermochronology, data compilation, deformation over geologic time

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SCG57-P05

Room:Convention Hall

Time:May 27 18:15-19:30

Formation and development of incipient shear zone in the lower crust: Example from theHasvik gabbro, Norway
KIMURA, Takafumi1∗ ; OKUDAIRA, Takamoto2
1

Department of Geosciences, Faculty of Science, Osaka City University, 2 Graduate School of Science, Osaka City University

Gabbroic rock is a major constituent of the lower crust, and it consists mainly of plagioclase and pyroxene. Although dislocation creep of plagioclase has generally been considered to govern the rheology of the lower crust, when the grain size ofthe constituent minerals is small enough, grain-size-sensitive creep dominates the mechanical behavior of the lower crust. The
process of grain-size reduction is a fundamental factor in controlling the strength of the lower crust. Instead of dynamic recrystallization, the nucleation that results from the fracturing and crushing of minerals have to be considered as potentially important
processes. In this study, to clarify the initial process of shear zone formation in the lower crust, we describe microstructural andpetrological characteristics of shear zones developed in the Hasvik gabbro of the Seiland Igneous Province in northern Norway(e.g., Tegner et al., 1999).
Shear-zone networks are developed in the Hasvik gabbro, and the shear zones are made up of fine (a few tens of microns),
equant, but slightly elongate grains of the recrystallized plagioclase, amphibole and pyroxene. On the other hand, in the primary magmatic crystals of plagioclase and pyroxene, intragranular and intergranular fractures are found. Newly crystallized
amphiboles are found along the boundaries between magmatic plagioclase and pyroxenes, in the intragranular fractures within
pyroxenes, and at the margins of pyroxene porphyroclasts in the shear zones. Recrystallized grains of plagioclase, clinopyroxene,
and orthopyroxene have compositions that differ from the magmatic ones, which suggests they formed by nucleation and growth.
Based on conventional plagioclase-amphibole thermobarometry (Holland and Blundy, 1994; Bhadra and Bhattacharya, 2007),the shear zones have formed at temperatures and pressures of 750-800 ℃, 0.8±0.2 GPa. The observed primary minerals cut by
fractures suggest high-temperature fracturing in the absence of high pore pressures, which implies a high strength of the lower
crustal gabbros and high stresses at fracturing. The viscously deformed shear zones are characterized by the lack of crystallographic preferred orientation (Okudaira et al., submitted) and a small grain size, suggesting that the mechanism of deformationof the fine-grained plagioclase and orthopyroxene has been diffusion accommodated grain-boundary sliding during and/or after
their nucleation and growth.

Keywords: gabbro, lower crust, brittle fracturing, grain-size reduction, grain-size-sensitive creep

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SCG57-P06

Room:Convention Hall

Time:May 27 18:15-19:30

Measurements of elastic wave velocity and electrical conductivity in a brine-saturated
granite under confining pressures
MAKIMURA, Miho1∗ ; WATANABE, Tohru1
1Graduate School of Science and Engineering, University of Toyama

Geophysical mapping of fluids is critical for understanding crustal processes. Seismic velocity and electrical resistivity structures have been revealed to study the fluid distribution. However, the fluid distribution has been still poorly constrained. Observed
velocity and resistivity should be combined to make a quantitative inference on fluid distribution. The combined interpretation
requires a thorough understanding of velocity and resistivity in fluid-saturated rocks. We have studied elastic wave velocities andelectrical conductivity in a brine-saturated granitic rock under confining pressures.
A fine grained (100-500 ?m) biotite granite (Aji, Kagawa Pref., Japan) was selected as a rock sample for its small grain size andtextural uniformity. Cylindrical samples (D=26 mm, L=30 mm) were heated to 100-600oC to increase the amount of crack (opengrain boundary), and filled with 0.1 M KCl aqueous solution. A linear relationship was found between the highest temperatureand the crack density parameter, which was estimated from velocities measured at atmospheric pressure. Velocity and electricalconductivity were simultaneously measured by using a 200 MPa hydrostatic pressure vessel. The pore-fluid was electricallyinsulated from the metal work by using plastic devices. The confining pressure was progressively increased up to 150 MPa,
while the pore-fluid pressure was kept at 0.1 MPa. It took 3 days or longer for the electrical conductivity to become stationary
after increasing the confining pressure.
Velocity and conductivity showed reproducibly contrasting changes with increasing confining pressure. Elastic wave velocities
increased by less than 10% as the confining pressure increased from 0.1 MPa to 50 MPa, while electrical conductivity decreasedby an order of magnitude. The changes were caused by the closure of cracks under pressure. The steep decrease in conductivity
at low pressures suggests that there are more cracks with smaller aspect ratios. Both velocity and conductivity showed no remarkable changes at higher pressures. An empirical relationship between the normalized conductivity and crack density parameter
was obtained. This relationship might be applied to a combined interpretation of seismic velocities and electrical resistivity.

Keywords: seismic velocity, electrical conductivity, resistivity, fluid, crack

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SCG57-P07

Room:Convention Hall

Time:May 27 18:15-19:30

Measurements of elastic wave velocity and conductivity in a brine-saturated sandstoneunder confining pressures
NAMBU, Minako1∗ ; WATANABE, Tohru1
1Department of Earth Sciences, University of Toyama

Geophysical mapping of fluids is critical for understanding crustal processes. Seismic velocity and electrical resistivity structures have been revealed to study the fluid distribution. However, the fluid distribution has been still poorly constrained. Observed
velocity and resistivity should be combined to make a quantitative inference on fluid distribution. The combined interpretation
requires a thorough understanding of velocity and resistivity in fluid-saturated rocks. We have studied elastic wave velocities andelectrical conductivity in a brine-saturated sandstone under different confining and pore-fluid pressures.
Berea sandstone (OH, USA) was selected as a rock sample for its high porosity (˜20%) and permeability (˜10-13 m2). It ismainly composed of subangular quartz grains, with small amounts of feldspar grains. Microstructural examinations showed thatclay minerals (e.g., kaolinite) and carbonates (e.g., calcite) fill many gaps between grains. The grain size is 100-200 micrometers. Cylindrical samples (D=26 mm, L=30 mm) were saturated with 0.1 M KCl aqueous solution. Measurements have been
made using a 200 MPa hydrostatic pressure vessel, in which confining and pore-fluid pressures can be separately controlled. An
aqueous pore-fluid is electrically insulated from the metal work by using a plastic devices. Elastic wave velocity was measured
with the pulse transmission technique (PZT transducers, f=2 MHz), and electrical conductivity the four-electrode method (f=100
mHz - 100 kHz) to minimize the influence of polarization on electrodes.
Confining and pore-fluid pressures work in opposite ways. Increasing confining pressure closes pores, while increasing porefluid pressure opens them. For a given pore-fluid pressure, both compressional and shear velocities increase with increasing
confining pressure, while electrical conductivity decreases. When confining pressure is fixed, velocity decreases with increasing
pore-fluid pressure while conductivity increases. The closure and opening of pores can explain observed changes of velocity andconductivity. In contrast to a granitic rock, a brine-filled sandstone showed only relatively small changes in conductivity. These
contrasting behaviors might reflect the difference in pore geometry between two rock samples.

Keywords: seismic velocity, conductivity, resistivity, sandstone, fluid

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SCG57-P08

Room:Convention Hall

Time:May 27 18:15-19:30

Grain growth in sintered polycrystalline diopside
TSUBOKAWA, Yumiko1∗ ; ISHIKAWA, Masahiro1
1

Yokohama National Univercity

Grain growth kinetics were studied in sintered polycrystalline diopside. The starting material was prepared from two typesof diopside single crystals (Ⅰ:Ca0.99 Na0.01 Mg0.97 Fe0.03 Si2 O6 , Ⅱ:Ca0.97 Na0.02 Mg0.86 Fe0.13 Si2 O6 ). They were crushed andmilled to particle size of <1µm. The powders were pressed into cylindrical shape under a uni-axial pressure of 2.0 MPa for
10 minutes. The pellets were then sintered at 1130 - 1280 ℃ for 2h and 6h. As a result, grain size increased and the porosity
decreased with increasing sintering temperature or sintering time. The experimental data can be fit the following relation, Df n
‒ D0 n = kt where n is a constant, Df and D0 are the grain size at time t = t and t = 0 respectively, and k is a rate constant.
For the sintered polycrystalline diopside, the parameter log10 k (µmn /s) was determined to be -3.3 or -4.8 for n = 2.59 or 2.64
respectively.
Keywords: grain growth, sintering, diopside, polycrystalline

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SCG57-P09

Room:Convention Hall

Time:May 27 18:15-19:30

Tectonic provinces of the Northern Fossa Magna region depicted by means of the crustal
movement and seismic activity
IMAI, Yuki1∗ ; TAKEUCHI, Akira2
1

Graduate School of Science and Engineering for Education, University of Toyama, 2 Graduate School of Science and Engineering for Research, University of Toyama

In the Northern Fossa Magna (NFM), large crustal earthquakes had been occurred in 1847 (the Zenkoji Earthquake) and recently. Understanding the tectonic provinces of the upper crust is important in order to clarify the generation mechanism of thecrustal earthquakes. The purpose of this study is revealing the tectonic provinces of the NFM region depicted by means of theregional characteristics of the crustal activity. The author investigated the crustal movement and the depth of the seismogenic
layer by analyzing GNSS observation data and hypocenter data, respectively.
Velocity field and strain rate field were estimated by analyzing GNSS observation data of GEONET and University of Toyama,
from October 2007 to March 2011. The depth of the seismogenic layer was evaluated using the JMA unified hypocenter catalog
from January 2003 to March 2011. Noises and low-frequency events were removed from the catalog with hypocenters that focal
depth is shallower than 40 km and magnitude is larger than 0.1. Relocation and declustering process of the hypocenters were notconducted in this study. The depth of the seismogenic layer was evaluated by means of the methods of Ito and Nakamura (1998),
the depth which 10%, 50%, and 90% of hypocenter occur are defined as the upper, middle, and lower depth of the seismogenic
layer.
As the results, considerable lateral variation in the crustal activity was revealed in and around the Niigata-NFM region. The
strain concentrate zone consisted of the WNW-ESE trend contraction strain more than 0.15 ppm/yr distributes from the northregion of Niigata Prefecture to the central region of Nagano Prefecture, and this zone corresponds to the northeastern part of
the Niigata-Kobe Tectonic Zone (Sagiya et al ., 2000). The displacement direction in the horizontal velocity field changes fromeastward in the northwestern part of the Niigata-NFM region to northward in the southern part. The depth of the seismogenic
layer shows lateral variation of about 10 km beneath the NFM region, and the inland region with a relatively shallow depth of
the seismogenic layer corresponds the location of active volcanoes. Focal mechanisms of the shallow crustal earthquakes in the
NFM region show reverse fault type and strike-slip fault type. These different mechanisms indicate that seismotectonic stressvaries around this region.
These results suggest the existence of the geodetic and seismological tectonic boundary that trends to NE-SW direction andinclines toward the west. This tectonic boundary is located obviously on the west side of the geological tectonic boundary, theShibata-Koide Tectonic Line (Yamashita, 1970) and Tsunan-Matsumoto Tectonic Line (Kosaka, 1984), along the eastern marginof the Shin’etsu sedimentary basin. A conclusive model for the tectonic provinces of the Niigata-NFM region shows that thetectonic boundary separates the whole crust into two provinces which having different characteristics in the horizontal velocity
field, seismogenic layer depth, and surface geology. The lateral variation in the seismogenic layer along the geodetic and seismological tectonic boundary might be the cause of generating the shallow crustal earthquakes in the NFM region. In order to discuss
about the detailed tectonic provinces of the NFM region, it is necessary the crustal activity are evaluated by various observations
with high spatial resolution.

Keywords: tectonic province, tectonic boundary, Northern Fossa Magna, strain concentrate zone, seismogenic layer

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SCG57-P10

Room:Convention Hall

Time:May 27 18:15-19:30

Seismic survey around the largest slip area of the 2011 Tohoku-oki earthquakeAZUMA, Ryosuke1∗ ; HINO, Ryota2 ; OHTA, Yusaku1 ; MOCHIZUKI, Kimihiro3 ; YAMADA, Tomoaki3 ;MURAI, Yoshio4 ; ITO, Yoshihiro5 ; YAKIWARA, Hiroshi6 ; SATO, Toshinori7 ; SHINOHARA, Masanao3
1

RCPEVE, Tohoku Univ., 2 IRIDeS, Tohoku Univ., 3 ERI. Univ. of Tokyo, 4 ISV, Hokkaido Univ., 5 DPRI, Kyoto Univ., 6 NTOEV,
Kagoshima Univ., 7 Graduate School of Sci., Chiba Univ.

The slip amount during the 2011 Tohoku-oki earthquake exceeded tens meters at the near-trench region off Miyagi, though
few meters caused at off Sanriku (e.g., Iinuma et al., 2012). Such the spatial variation of the coseismic slip seems to reflect thevariation of the physical property on the interplate fault, which can be correlated with a seismic velocity structure. In this study,
to understand the mechanism of enormous coseismic slip of this megathrust event, we investigate the heterogeneity of the seismic
velocity structure around the fault.
Many seismic refraction surveys were carried out at off Miyagi and Sanriku regions. Azuma et al. (2013) found the high-Vp
anomaly in the overriding plate, corresponding the backstop block (Tsuru et al., 2002), at the area of 38?38.5N and 20 km fromthe trench axis (Figure 1). This Vp anomaly overlapped the large slip area during the 2011 earthquake, and they suggested thatthe heterogeneous structure in the overriding plate controlled the extent and amount of the coseismic slip near the trench basedon the 2-D structure model along a seismic profile. It is expected that similar correlation between the seismic velocity and theamount of coseismic slip is broadly observed in the trench slope area, if the coseismic slip was actually controlled by the material
heterogeneity, e.g. the distribution of backstop brock.
To confirm broad consistency of the previously identified structural variation, we conducted a seismic survey on October 2014
in the gap area where no seismic surveys have been conducted (Figure 1). We set two survey lines, with a length of 180 km,
which run slightly oblique against the Japan Trench axis. Along the profiles, 17 and 20 ocean bottom seismometers (OBSs) were
deployed. The spacings of the OBSs were 10 and 8 km, along the land-ward and trench-ward profiles, respectively, taking into
account the difference in depths to the plate interface. We used an airgun array composed of four guns with a total volume of
100 liters as a controlled source. During the shooting operation, we also collected near-vertical reflection data by a 48-channelhydrophone streamer with a length of 1.2 km.
The obtained wide-angle data showed clear first arrivals within the offset range of 60 km, and later phases interpreted as thewide-angle reflections from the plate interface. Further analyses of the obtained data set will provide a velocity structural model
to clarify more detailed distribution of the backstop block and to reinforce the interpretation based on the spatial correlation
between the high-Vp block and large coseismic slip area of the 2011 Tohoku-oki earthquake.

Figure 1. Map view of surveyed area. Red lines and yellow plots indicate survey lines and deployed OBSs ′ positions of thisstudy. Black line indicates the profile of Azuma et al. (2013). Blue arrow represents the high Vp area detected by Azuma et al.
(2013). Gray lines were surveyed by Ishihara et al. (2015). Black blocks shows the distribution of sedimentary prism obtained byreflection surveys (after Tsuru et al., 2002). Color-filled contour represents the coseismic slip distribution of the 2011 Tohoku-oki
earthquake (Iinuma et al., 2012).
Keywords: crustal structure, 2011 Tohoku-oki earthquake

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SCG57-P10

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SCG57-P11

Room:Convention Hall

Time:May 27 18:15-19:30

Grain growth of nanocrystalline labradorite
HONDA, Satoko1∗ ; ISHIKAWA, Masahiro1
1

Yokohama National University

Plagioclase is a solid solution series that ranges from albite to anorthite endmembers (with respective compositions NaAlSi3 O8
to CaAl2 Si2 O8 ). Plagioclase is a major constituent mineral in the Earth’s crust. Its physical and chemical properties are importantfor establishing the overall rheology of Earth’s crust. Previous experimental studies on sintering on plagioclase were mostly
concentrated on the endmembers under the high-pressure conditions, thus there are few reports on sintering of plagioclase withintermediate composition.
In this study, sintering of labradorite polycrystalline were performed by using nanoscale powders of natural labradorite, andgrain growth kinetics was studied in sintered polycrystalline labradorite. We prepared nanoscale mineral powders from natural
crystals of labradorite (Ab38An62) by milling. Sintering experiments were carried out at a temperature of 1100-1210 ℃ with
controlling time after milling and formed mineral powders. Starting materials were characterized by electron probe micro analysis(EPMA). The resultant materials were characterized by X-ray powder diffraction (XRD), secondary electron microscope (SEM)and Xray fluorescence (XRF) analysis.
Grain growth occurred with increasing sintering temperature or sintering time. The experimental data can be fit the following
relation, Df n -D0 n = kt where n is a constant, Df and D0 are the grain size at time t = t and t = 0 respectively, and k is a rate
constant. For sintering, a temperature of 1100-1210 ℃ with controlled time can provide high dense aggregates of labradorite withan average grain size of 0.5micro m, porosity of 3vol% and volume reduction of 60%. In this study, we found that high dense
and fine grain polycrystalline Labradorite can be made from nano-sized powders (<100nm) by atmospheric pressure sintering.

Keywords: plagioclase, sintering, grain growth

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SCG57-P12

Room:Convention Hall

Time:May 27 18:15-19:30

Effects of seismic velocity anomaly zone below Northeast Japan on displacement of the2011 Tohoku earthquake
HASHIMA, Akinori1∗ ; BECKER, Thorsten2 ; FREED, Andrew3 ; SATO, Hiroshi1 ; OKAYA, David2 ;SUITO, Hisashi4 ; YARAI, Hiroshi4 ; MATSUBARA, Makoto5 ; TAKEDA, Tetsuya5 ; ISHIYAMA, Tatsuya1 ;IWASAKI, Takaya1
1

Earthquake Research Institute, University of Tokyo, 2 University of Southern California, 3 Purdue University, 4 Geospatial Information Authority of Japan, 5 National Research Institute for Earth Science and Disaster Prevention

2011 M9 Tohoku earthquake, Japan, has the 500-km long and 200-km wide source region and large deformation was observed
over the Japanese islands. Japan is deployed with dense GPS observation network. Analyzing the spatial features of the crustal
deformation data, we can obtain not only information of the source of the Tohoku earthquake but also that of crustal structure.
The Northeast Japan arc is formed by the subduction of the Pacific plate below the Eurasian plate. The volcanic front is locatedalong the Ou Range. Studies of seismic tomography has revealed low velocity region below the volcanic front due to the intrusionof hot materials and high velocity region below the Pacific coast due to crustal thinning and ascending of mantle materials. In
this study, we construct a finite element model incorporating 3-D crustal structures and examine the effect of crustal heterogeneity on the surface deformation using slip distribution obtained from inversion of the surface displacements due to the Tohoku
earthquake. We utilize the large, land-based Japan GPS array as well as seafloor geodetic constraints in the inversion. Our FEM
considers a region of 4500 km x 4900 km x 670 km, incorporating the Pacific and the Philippine sea slabs by interpolating
models for the Tohoku region and the Nankai trough, as well as the Kuril, Ryukyu and Izu-Bonin arcs. As the geometry of theplate boundaries, we used the model interpolating the existing local plate boundary models. The model region is divided into
about 500,000 tetrahedral elements with average dimension ranging from 5-100 km. We also test the role of gravity on coseismic
results, with initial results suggesting that gravitational loading is not an important factor because of the shallow dip of the upper
Pacific slab. As for the elastic structure, we used PREM model. To represent high and low velocity zone under the Pacific coastand volcanic front, respectively, we introduced 80-km thick region in the model. We also computed with the associated layered
structure model to check the effect of crustal heterogeneity. We obtained almost the same slip distribution for both the layered andcrustal heterogeneity models, indicating that the deviation of the displacement due to crustal heterogeneity from layered model
does not affect slip inversion. Using these results, we calculated surface deformation for models. We compared the two results bypatterns of residual displacements, which is obtained by subtracting computed displacements from observed displacements. In
the case of layered model, most of Northeast Japan shows eastward residual vectors and the westward vectors can be found along
the Pacific coast. These residuals are diminished in the crustal heterogeneity model, so this model better explains the observation.
In this way, we can extract information of detailed elastic structure by using broad surface deformation field data. This will allow
us to calculate more realistic stress state in the crust.
Keywords: 2011 Tohoku Earthquake, Crustal deformation, Finite element modeling, Seismic velocity structure, Northeast Japanarc, Active fault

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SCG57-P13

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A method to estimate friction coefficient from orientation distribution of meso-scale faults
SATO, Katsushi1∗
1Div. Earth Planet. Sci., Kyoto Univ.

Static friction coefficient controls the brittle strength of earth’s crust of which deformation is recorded as faults. It is difficult
to estimate the friction coefficient of ancient geological faults because fault gouge does not preserve its physical property. This
paper proposes a method to determine friction coefficient from orientation distribution of fault planes.
Stress tensor inversion techniques have been applied to geological meso-scale faults to calculate a reduced stress tensor, whichis composed of three principal stress orientations and a stress ratio. Angelier (1989) tried to determine all six independent components of stress tensor including magnitudes of principal stresses, assuming that the ratio of normal and shear stresses on observed
fault surfaces exceeds the friction coefficient. The assumption allows us to estimate the friction coefficient of meso-scale faults
as the slope of linear boundary of distribution of points representing normal and shear stresses on Mohr’s diagram. However,there has been remained uncertainty in the estimation since the recognition of the line has been done manually on the diagram.
This study computerizes the estimation of friction coefficient as follows. Meso-scale faults are assumed to slip when they satisfy the cohesionless Coulomb’s failure criterion represented by the linear friction envelope. The principal stress axes and stressratio are presumed to be stable, while the changes in the magnitude of differential stress and the fluid pressure are taken into
account. When the two parameters fluctuate to cause faulting, the Mohr’s circle moves to leftward (negative direction of effective
normal stress). Then, a upper left part of the Mohr’s circle is cut off by the friction envelope and the faults corresponding to thepart are activated. If such events are repeated with various values of differential stress and fluid pressure, the orientation distribution of activated faults should have concentration around the tangential point between the friction envelope and the Mohr’s circle
normalized to satisfy sigma 1=1 and sigma 3=0. According to the above-mentioned concept, the new method searches for the
direction of linear gradation in the frequency of fault planes on the normalized Mohr’s diagram. The slope of friction envelope isgiven by linear contour lines of frequency of faults.
The method was applied to natural fault-slip data gathered from the Pleistocene Kazusa Group, eastern Boso Peninsula. The
strata are composed of sandstones and slitstones. Stress inversion analysis (Sato, 2006) gave a WNW-ENE trending tensional
stress. The friction coefficient was determined to be 0.66 +0.05/-0.05, which is typical value for sandstone.
References
Angelier, J., 1989, Jour. Struct. Geol., 11, 37-50.
Sato, K., 2006, Tectonophys., 421, 319-330.

Keywords: stress tensor inversion, fault-slip analysis, friction coefficient, orientation distribution

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SCG57-P14

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Landward migration of active folding estimated from topographic developments along theeastern margin of the Japan Sea
OTSUBO, Makoto1∗ ; MIYAKAWA, Ayumu1
1Geological Survey of Japan/AISTThe Quaternary tectonics of the Japan arc is characterized by strongly crustal deformation, whose mode and rate are quite
different from those of the preceding late Pliocene. The Tohoku district, on the eastern margin of the Japan Sea, lies withina strongly compressive area that has been experiencing large, contractional, crustal deformations, since the late Pliocene (Satoand Amano, 1991). Fold-and-thrust structures (Sato, 1989) and fold-topographic structures with distributed reverse faults (e.g.,
Okamura et al., 1995) have developed in response to this contractional deformation. Geodetic surveys in the Tohoku district
have detected zones with a high rate of horizontal strain (Sagiya et al., 2000). When the contractional deformation continues tothe present, the high strain rate zones at the geological and geodetic scales should be overlapped. However, the high horizontal
strain-rates recognized at geological and geodetic time-scales are spatially heterogeneous. Rates are consistent in the Niigata
region, in the southwestern part of the Tohoku district, but not in the Akita region in the northwestern part of the district. Thereis, therefore, a need to constrain the spatial differences in the horizontal strain-rate between the geological and geodetic timescales, in order to understand regional tectonic differences across the district.
We focus here on the erosional and topographic evolution of fold structures developed since the late Pliocene in the Akita
and Niigata regions. We measured the distance between the fold hinge lines and the mountain ridge lines. We targeted 44 folds
that were activated since the late Pliocene, comprising 12 and 32 folds in the Akita and Niigata regions, respectively. Spatial
variations in the normalized deviations are consistent with the systematic eastward migration of fold growth in the area. The
topographic behavior indicates that the landward migrating of the fold growth is generally constant.
References: Ellis, M.A., Densmore, A.L., 2006. Geological Society of America Special Papers 398, 251-266; Lave, J.,
Avouac, J.-P., 2000. Journal of Geophysical Research: Solid Earth 105 (B3) 5735-5770; Merritts, D., Ellis, M., 1994. Journal ofGeophysical Research: Solid Earth 99 (B6), 12135-12141; Okamura, Y., Watanabe, M., Morijiri, R., Satoh, M., 1995. Island Arc4, 166-181; Sagiya, T., Miyazaki, S., Tada, T., 2000. Pure and Applied Geophysics 157, 2303-2322; Sato, H., 1989. Memoirsof the Geological Society of Japan 32, 257-268; Sato, H., 1994. Journal of Geophysical Research: Solid Earth 99 (B11), 2226122274; Sato, H., Amano, K., 1991. Sedimentary Geology 74, 323-343; Sibson, R.H., 2009. Tectonophysics 473, 404-416.

Keywords: fold, fault, topography, earthquake, deformation, high strain rate zone

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SCG57-P15

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Block-in-matrix fabric by frictional grain-boundary sliding of the Hioki melange of Shimanto belt, Shikoku, JapanTABUCHI, Yu1∗ ; TONAI, Satoshi1
1Graduate School of Integrated Arts and Science, Kochi University

We report lithology, deformation structures, and clay mineral contents of the Hioki melange, which constitutes part of theyoungest (late Oligocene to early Miocene) portion of the Shimanto accretionary complex, Shikoku, Japan. The Hioki melange
is comprised essentially of a dark gray shaly matrix that envelops blocks and large rafts of mainly sedimentary rock. Although
it is regarded as accreted within a few kilometers below the surface (e.g., Hibbard et al., 1993; Underwood et al., 1993), thedeformation process of the melange still remains unclear. The deformation mechanism of the melange is essential information tounderstand this problem.
The lithology and deformation structures are observed using core samples and outcrops along coastline at Muroto, Kochi,
Japan. The core samples were collected at two localities (HK01 and HK02) and are about 40 m length, respectively. The wholeof the samples show block?in?matrix fabrics. The ratios of the blocks change irregularly between 0 to 40 %. Furthermore,some fracture zones are observed throughout the samples. Some of these fracture zones contain clay minerals. In the field,
block?in?matrix fabrics are also observed throughout the study area. The size of blocks ranges from millimeter to meter scale.
There were three shapes in the blocks, which are brecciated, boudinage, and layered blocks. Some blocks are injected by shale.
The matrix, which is partly folded, is composed of dark gray shale and some green tuff and dark brown shale. Microscopic
observation revealed that the shear displacement of the matrix has been achieved by grain boundary sliding and some pressure
solution. Attitudes of bedding plane, cleavage foliation, and major axis of boudinage blocks are parallel in many cases.
Clay mineral contents were investigated by XRD analysis on 23 samples (7 samples for HK01, 5 samples for HK02, and 11
samples for outcrops) throughout the study area. The result shows that illite is the major mineral in all samples. In addition,
chlorite is contained in the samples of HK02 and the northern half of outcrop, and kaolin minerals are contained in the fracturezone.
Two possible explanation are concerned for the process of the block-in-matrix fabric of the Hioki melange. One explanationis that this fabric has formed under the condition that the contrast in competence between the sand (block) and the shale (matrix)
is relatively high. In this case the sand layers have consolidated and deformed by brittle failure, although the shale layers have
deformed by grain boundary sliding. In this case, blocks from same layer should form a line. It is a future problem to confirm.
Another explanation is that host strata of the Hioki melange have deposited as mud layer with some boulders. In this explanation,
sandstone blocks may have been transported by debris flow and/or submarine landslide. On the other hand, the fracture zones
have formed in the consolidated melange, which have been uplifted to shallower part of the accretionary prism.

Keywords: block-in-matrix fabric, grain boundary sliding, Shimanto belt, melange

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SCG57-P16

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Changes in seismic velocity and electrical conductivity in a brine-saturated granite under
uni-axial compression
MORIMOTO, Misaki1∗ ; WATANABE, Tohru1
1Department of Earth Sciences, University of Toyama

Geophysical observations have shown that fluids exist pervasively within the crust. Fluids are mainly situated at intra-graincracks and open grain boundaries. Since the opening of cracks strongly depends on the stress state, bulk properties such as seismic
velocity and electrical conductivity, which are strongly affected by fluid-filled cracks, should be anisotropic under a stress state.
In order to understand the anisotropy in velocity and conductivity under stress, we have been constructing an experimental system
for studying the anisotropy in elastic wave velocity and electrical conductivity in a brine-saturated granitic rock under uni-axial
stress.
The loading system is composed of a hand press (Maximum load: 20 kN), a load cell and stainless steel end-pieces, whichcontains ultrasonic transducers for velocity measurements in the axial direction. A fine grained (100-500 ?m) biotite granite (Aji,Kagawa Pref., Japan) was selected as a rock sample for its small grain size and textural uniformity. A cylindrical sample (D=26mm, L=30 mm), to the cylindrical surface of which ultrasonic transducers are mounted for velocity measurements in the radial
direction, is assembled with end-pieces, and then loaded. One compressional wave velocity and two shear wave velocities canbe measured in the axial and two radial directions. Electrical impedance can also be measured in the axial and radial directions.
Preliminary runs on a dry rock sample have showed that velocities in the axial direction increased significantly with the axial
compression. No significant change was observed in velocities propagating in the radial directions. These observations can be
explained by the closure of cracks perpendicular or subperpendicular to the compression axis. Experiments on wet samples will
also be reported in this poster.

Keywords: seismic velocity, electrical conductivity, anisotropy, fluid, compression, stress

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SCG57-P17

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Detrital zircon chronology of the Upper Cretaceous Atokura Formation in northern Kanto
Mtn., Japan
NAKAHATA, Hiroki1∗ ; ISOZAKI, Yukio2 ; KOSAKA, Kazuo3 ; SAKATA, Shuhei4 ; HIRATA, Takafumi4
1

Department of Earth and Planetary Science, Graduate School of Science, The Univeristy of Tokyo, 2 Department of Earth
Science and Astronomy, The University of Tokyo, 3 Department of Geosystem Sciences, College of Humanities and Sciences,
Nihon University, 4 Graduate school of Science, Kyoto University
The Cretaceous sandstones of the Atokura nappe in the northern Kanto Mtns. in central Japan were analyzed for detrital zircon
U-Pb chronology by LA-ICP-MS. The results documented two distinct age groups; i.e., 150-300 Ma (Permian to Jurassic) and
1600-2600 Ma (Neoarchean to Mesoproterozoic). As there are no correlative candidates for provenance in the neighborhood,
the Cretaceous strata of the Atokura nappe were likely exotic. The occurrence of Jurassic granitoids is currently limited to the
Hida belt in central Japan, while no Precambrian basement is exposed at all in Japan. Judging from the allochthonous mode ofoccurrence, the Atokura nappe was derived originally from the back-arc domain of the Cretaceous Japan.

Keywords: Cretaceous, sandstone, detrital zircon, U-Pb age, LA-ICP-MS, Japan

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SCG57-P18

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Dislocation creep induced layer structures ? in mafic rocks, Tanzawa Mountain
MIZUNO, Tomoki1∗ ; MICHIBAYASHI, Katsuyoshi11Institute of Geosciences, Shizuoka University

Tanzawa plutonic complex is located in the northen part of Izu-Bonin-Mariana (IBM) arc. The complex has been exposed by
the collision of IBM arc and Japan islands. The exposed process is related to uplifting of Tanzawa plutonic complex along the
Kannawa fault. Mafic rocks near the Tanzawa plutonic complex show metamorphosed and deformed textures. The purpose of thisstudy is to reveal microstructures of metamorphosed mafic rocks occurred near the Tanzawa plutonic complex. They are highly
deformed and show well-developed layer structures. The mafic rocks consist mainly of amphibole and plagioclase. Amphibole
grains are elongated. Plagioclase grains are polygonal. The mean grain sizes of amphibole are in a range between 30 and 110
micron, whereas those of plagioclase are in a range between 25 and 115 micron. Within the well layered rocks, aspect ratios
become smaller, as increasing grain sizes. Crystal-preferred orientations (CPOs) of amphibole and plagioclase were measured
by a scanning electron microscope (SEM) equipped with electron back-scattered diffraction (EBSD). Amphibole CPOs show(100) [001] patterns. Plagioclase CPOs show (001) [100] patterns. It suggests that their deformation mechanisms are dominantly
dislocation creep. Some elongated amphibole grains have grain boundaries perpendicular to the foliations, which appear to bealso an evidence of dislocation creep. Consequently, the mafic rocks could result from dislocation creep during the developmentof layer structures associated with uplifting of the Tanzawa plutonic complex.
Keywords: amphibolite, Tanzawa, amphibole, plagioclase, CPO

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SCG57-P19

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Brittle and ductile textures preserved in Kashio mylonite along the Median Tectonic Line,
Sakuma-cho, Shizuoka
ENDO, Hiroto1∗ ; MICHIBAYASHI, Katsuyoshi11Institute of Geosciences, Shizuoka University

Kashio mylonite exposed along the Median Tectonic Line in the central Japan is one of the most famous fault rocks inJapan. The purpose of this study is to reveal microstructural development of Kashio mylonites in the Urakawa area,Sakumacho, Shizuoka Prefecture. Kashio mylonite occur along the Ohchise-gawa River and Shippei-sawa. In this study, four Kashio
mylonites were classified into three types: protomylonite, mylonite, and ultramylonite. The whole rock chemical compositions
show that they were derived from the igneous rocks such as tonalites. Two protomylonites have larger (˜4mm) plagioclase andamphibole porphyroclasts and show composite planar structures. The plagioclase porhyroclasts were fractured but partly dynamically recrystallized into fine-grains. All quartz grains were dynamically recrystallized into fine (about 40 micron) grains.
One mylonite consists of very fine-grained quartz (about 20 micron) and plagioclase bands with small amount of plagioclase
porphyroclasts. One ultramylonite consists of very fine-grained matrix of quartz, plagioclase and K-feldspar (about 10 micron).
Ultramylonite were fractured such as cataclasitic rocks after the mylonitization. Crystal-preferred orientations (CPO) of quartz
were measured in the four mylonitic samples. Quartz CPO patterns suggest that prism <a>slip system is dominant, whereas theultramylonite have a weak cross girdle pattern of c-axis. It suggests that the ultramylonite was progressively developed during
deformation under the retrogressive condition. As a result, these mylonitic rocks have undergone three stages of the deformation
event. The first stage of deformation occurred in the ductile regime of plagioclase, resulting in the fine-grained plagioclase andY-maxima CPO patterns of quarts c-axes. The second stage of deformation occurred in the brittle regime of plagioclases, resulting in fracturing within plagioclase porphyroclasts and the weak cross girdle CPO pattern of quartz c-axis in the ultramylonites.
Finally, the third stage of deformation occurred in the brittle regime of both quartz and plagioclase, resulting in the developmentof cataclasite. The results support that the Kashio mylonites have been deformed during progressive retrogression associatedwith the development of Median Tectonic Line.
Keywords: Median Tectonic Line, Kashio mylonite, CPO, ductile regime, brittle regime

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SCG57-P20

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Thickness of seismogenic layer within the crust on the Japan Sea side
MATSUBARA, Makoto1∗
1

NIED

1. Introduction
We investigate the depth of the seismogenic layer in order to estimate the lower limit of the seismogenic fault plane since thisdepth is related to the size of the earthquake caused by the active fault. We have index D10 and D90 as the upper and lower limitof seismogenic layer, respectively. D10 is defined as the depth above which 10 % of the whole crustal earthquakes occurred fromthe surface. D90 is the depth above which 90 % of the crustal earthquakes occurred from the surface. The difference between the
D10 and D90 is the thickness of the seismogenic layer.
2. Data and method
NIED Hi-net has a catalog of hypocenters determined with one-dimensional velocity (1D) structure (Ukawa et al., 1984).
We construct the system to relocate the hypocenters from 2001 to 2013 with magnitude greater than 1.5 on the Japan Sea side
shallower than 50 km depth with three-dimensional velocity (3D) structure (Matsubara and Obara, 2011). We estimate the D10
and D90 from the hypocenter catalog with 3D structure.
3. Result
The many earthquakes determined shallower than the 5 km with 1D structure are relocated to deeper with 3D structure and theearthquakes deeper than 15 km are relocated to about 5 km shallower. D10 becomes deeper and D90 becomes shallower with 3D
structure.
From Akita to Niigata prefecture, D90 is deeper than the other area and D90 beneath the Japan Sea is much deeper than theinland area. The thickness of the seismogenic layer in this area is also thick from 8-16 km. On the west side of the area, D90 isvery shallow as 11-16 km and the thickness of the seismogenic layer is also thin as 2-7 km from Toyama to Tottori.
4. Discussion
Omuralieva et al. (2012) relocated the JMA unified hypocenters with 3D structure. D90 became shallower than that from the
JMA catalog. Very deep D90 beneath the northern Hokkaido and from Akita to Niigata is consistent with our result.
5. Conclusion
Using 3D structure, the depth of shallow earthquakes is relocated to deeper and that of the deep earthquakes is relocated toshallower then D10 deepens, D90 shallow, and the thickness of the seismogenic layer becomes thinner. The thickness of theseismogenic layer is thick beneath the region from the Akita to Niigata prefecture on the northeastern Japan Sea side, however,that is very thin beneath the region from Toyama to Tottori prefecture on the west side of the Japan Sea coastal area.
Keywords: seismogenic layer, D90, D10, seismic fault

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SCG57-P21

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P-wave velocity structure at shallow depths around the northern limit of the 2011 Tohoku
earthquake
ISHIHARA, Ken1∗ ; MOCHIZUKI, Kimihiro1 ; YAMADA, Tomoaki1 ; YAMASHITA, Yusuke1 ; SHINOHARA, Masanao1 ;AZUMA, Ryosuke2 ; HINO, Ryota3 ; SATO, Toshinori4 ; MURAI, Yoshio5 ; YAKIWARA, Hiroshi6
1Earthquake Research Institute, The University of Tokyo, 2 Recearch Center for Prediction of Earthquake and Volcanic Erupstion,
Tohoku University, 3 International Research Institute of Disaster Science, Tohoku University, 4 Graduate School of Science, Chiba
University, 5 Faculty of Science, Hokkaido University, 6 Faculty of Science, Kagoshima University
Before 2011 Tohoku earthquake, some seismic surveys had been conducted within the co-seismic slip area of the earthquake.
However structures may have been changed after the earthquake due to the co-seismic slip. We need to compare the structuresof the same area of different times in order to reveal changes caused by the 2011 Tohoku earthquake. Therefore, a refractionreflection seismic survey was conducted in 2013 at the same area of the 1999 and 2001 surveys. Seven 100 km long profiles
were surveyed parallel to the Japan Trench. Forty-four OBSs were deployed and hydrophone streamer was towed behind theshooting vessel. Air-gun array was used as controlled seismic sources. Because the area of 2013 survey includes the co-seismic
slip area of the 2011 Tohoku earthquake, the changes of structure may be revealed by comparing results of 1999 and/or 2001
survey with that of the 2013 survey. Especially the profiles include the northern limit of the co-seismic slip area of the 2011
Tohoku earthquake in their north, so it may be possible to put constraints on the northern limit.
We could identify some differences on the seismic reflection sections and in the recorded waveforms between the 2001 and2013 surveys. It is, then, expected to reveal some structural changes before and after the 2011 Tohoku earthquake.
We constructed 1-D V-p structures to about 2km depth beneath the seafloor for each OBS station by applying the Tau-P method.
Then we constructed 2-D V-p structure models by referring to the 1-D V-p structures for profiles so that the models explain travel
times of shallow P-wave arrivals.
Keywords: the northern limit of the 2011 Tohoku earthquake, controlled source seismic survey, ocean-bottom seismometer(OBS)

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SCG57-P22

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Seismic basement structure in and around the northeastern Kanagawa Prefecture inferredfrom the seismic interferometry
MIZUHO, Yamazaki1∗ ; YOSHIMOTO, Kazuo1 ; NAKAHARA, Hisashi2 ; SAKAI, Shin’ichi3 ; HIRATA, Naoshi3
1Graduate School of Nanobioscience, Yokohama city University, 2 Graduate School of Science, Tohoku University, 3 Earthquake
Research Institute, University of Tokyo
1. Introduction
Detailed information on seismic basement structure is required for understanding the formation process of the Kanto sedimentary basin. In this study, we investigated the seismic basement structure in and around the northeastern Kanagawa Prefectureby the pseudo reflection seismic profiles from the seismic interferometry of local earthquake waveforms, with other geophysicalinformation from geophysical exploration and deep borehole observation.
2. Data and Analysis
Twenty-seven thousand seismic waveforms of the local earthquakes recorded by SK-net, K-NET, and MeSO-net, were analyzed in this study. Following Yoshimoto et al. (2009), we analyzed the SH displacement waveforms of moderate size earthquakes. After the calculation of the autocorrelation functions of each SH displacement waveform with a length of 10s from theS-wave onset, autocorrelation functions from all events were stacked at each station to obtain the reflection response of S-wave
for shallow underground structure.
3. Result
We found clear reflective surfaces in the pseudo reflection seismic profiles. As for the Atsugi-Yokohama survey line, it was
found that significant reflective surface is inclined to the east from 2s to 6s in two-way tarveltime. We interpreted this reflective
surface as the top of the Shimanto belt, comparing the geological information at Sagamihara borehole (Ozawa et al., 1999). The
observation stations located at the north of the Tama River show very reflective surface compared with those located above the
Shimanto belt. Since this reflective surface is observed at the vicinity of Koto borehole and Fuchu borehole, we interpreted thisreflective surface as the top of the Chichibu belt.
The boundary of the Shimanto belt and the Chichibu belt is found to be located nearly along the Tama River, slightly shifting
to the south near the northeastern Yokohama City. The top of the Shimanto belt in the south side of this boundary was foundat 6s in two-way tarveltime in the mideastern Yokohama City, and it is about 1s deeper than the top of the Chichibu belt in
the north side. It was also found that the Shimanto belt becomes shallower toward the west in western Yokohama City (in andaround Asahi-ku and Totsuka-ku). These results are consistent with the seismic traveltime analysis (Yokohama City, 2000). As
for the top of the Chichibu belt, it’s depth was estimated to be nearly horizontal in the east of Chofu, Tokyo, however, it becomessuddenly shallower at the westward of Fuchu.

ACKNOWLEDGMENTS
Data provided by SK-net, K-NET, and MeSO-net are gratefully acknowledged. We thank Tokyo metropolitan government,
Chiba and Kanagawa Prefecture, and Yokohama City. We also thank the National Research Institute for Earth Science and Disaster Prevention and the Japan Meteorological Agency.

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SCG57-P23

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Seismic reflection profiling off-Tottori and Fukui, SW Japan, for seismic and tsunami
hazards in the Sea of Japan
KATO, Naoko1∗ ; SATO, Hiroshi1 ; ISHIYAMA, Tatsuya1 ; SHIRAISHI, Kazuya2 ; ABE, Susumu2
1

ERI, Univ. of Tokyo, 2 JGI. Inc.

To estimates Tsunami and seismic hazards along the coastal area of Sea of Japan, more detailed survey to identify source faults
are needed. A research project funded by MEXT named ”the integrated research project on seismic and tsunami hazards aroundthe Sea of Japan” began in FY 2013. To obtain the information of source faults, we performed deep seismic reflection profilingoff-Fukui and Tottori area in the southwestern part of Honshu, Japan. Multi-channel seismic reflection data were acquired alongfour seismic lines in off-Fukui area and five seismic lines off-Tottori in the area within 50 km distance from the shoreline. Total
length of seismic line is 190 km in off-Fukui and 280 km in off-Tottori. We used two vessels; a gun-ship with 3020 cu. inch airgun and a cable-ship with a 2-km-long, streamer cable with 168 channels and 1050 cu. inch air-gun. The survey area consists ofstretched continental crust and marked by densely distributed syn-rift normal faults. The thickness of Neogene basin fill is 5 km
in off-Tottori and 3 km in off-Fukui. The rift basin fill along the arc-parallel normal faults were strongly deformed in late Miocene
by basin inversion. The gently dipping Pliocene sediments cover the folded strata unconformably. Some of the Miocene reverse
faults displaced late Pliocene sediments. Latest fault system is high-angle faults, whose displacement is preserved in topographic
features. Judging from the patter of reflection the fault system is strike-slip faults.

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SCG57-P24

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Crustal deformation in Hokkaido after the 2003 Tokachi-oki earthquake using GNSS data
ITOH, Yuji1∗ ; NISHIMURA, Takuya2
1

Graduate School of Science, Kyoto University, 2 Disaster Prevention Research Institute, Kyoto University

The Tokachi-oki earthquake (Mw = 8.0) occurred on the plate interface along the Kurile trench on 26 September 2003. Largeinterplate earthquakes like this are generally accompanied by the postseismic deformation. Postseismic deformation of thisearthquake is well observed by GNSS. It is proposed that afterslip and viscoelastic relaxation are dominant mechanisms for thepostseismic deformation. Afterslip is aseismic slip that occurs in and around the slip area of the mainshock. It lasts for several
days to several years. Viscoelastic relaxation is the crustal deformation caused by flow of viscoelastic material due to the changeof stress distribution. It lasts for several years to several decades and its effect is more widely distributed than that of afterslip [e.g.
Scholz, 2002]. The effect of viscoelastic relaxation should be eliminated from the observed data when we infer the interplate
coupling, especially its healing process after the mainshock, so an estimation of that is important. Theoretically, we can use
a difference of relaxation times between two mechanisms to eliminate it, but we don’t know when it actually starts to play adominant role in postseismic crustal deformation.
Several previous studies, such as Miyazaki et al. (2003), Ozawa et al. (2004), and Baba et al. (2006) inverted the observed
displacement data and inferred the afterslip distribution of this earthquake. Tanaka (2007) showed that the effect of viscoelastic
relaxation is detectable in the observed data by a forward calculation. However, all of them use the data observed for only 2 years
after the event, so we analyze the crustal deformation data for 7 years after the event observed by GNSS at the GEONET stations
and investigate the effect of both afterslip and viscoelastic relaxation. We, here, describe the feature of the observed deformation
after the Tokachi-oki earthquake.
Before the calculation of the deformation velocity after the event, we eliminate linear trends and the significant coseismic
displacement of 3 earthquakes occurred near Hokkaido on 15 November 2006, 11 September 2008 and 5 June 2009 [Kimura &Miyahara, 2013]. We estimate the velocity by piecewise linear approximation. The horizontal velocity is estimated every year.
The vertical velocity is estimated every year for first 3 years after the earthquake and every 2 years for the remaining period.
The observed data in the Tokachi, the Kushiro and the Nemuro regions were affected by double Kushiro-oki earthquakes on
29 November and 6 December 2004 (M = 7.1, 6.9, respectively). The postseismic deformation of these earthquakes lasted for
2 years in the eastern Tokachi, the Kushiro and the Nemuro regions near the hypocenter. In the western Tokachi region, thepostseismic deformation lasted for 1 year. From 3 years after the Tokachi-oki earthquake, vertical velocity in the Tokachi andKushiro regions was larger than that of in the stations near Cape Erimo, so we propose that the effect of viscoelastic relaxation
was increasing there relatively and/or afterslip area moved to northeast.
In the Douou region, that is northwestern region of hypocenter, from 4 years after the mainshock, spatial decay of horizontal
velocity is notably smaller than that in the northern and northeastern regions.
From examining the data analysis, we concluded that viscoelastic deformation started to play a dominant role in postseismic
deformation after 3 years following the mainshock. We assumed a 2-layers structure model consisting of an elastic layer overlying
a viscoelastic half-space and estimated the thickness of the first layer and the viscosity of the half-space by grid search. As apreliminary result, we obtained 60 km and 8.0 × 1018 Pa s for the elastic thickness and the half-space viscosity, respectively. The
viscoelastic model almost explains the deformation in the northwest and southeast region of Asahikawa.
Acknowledgments: We used the GNSS data(F3 solution) provided by GSI.

Keywords: postseismic crustal deformation, viscoelastic relaxation, 2003 Tokachi-oki earthquake, GNSS

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SCG57-P25

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Moho discontinuity beneath the Japanese Islands inferred from grid search analysis ofreceiver functions
IGARASHI, Toshihiro1∗ ; IIDAKA, Takashi1
1

ERI, Univ. of Tokyo

Information on seismic velocity and seismic velocity discontinuities is important to clarify the characteristics of the seismogenic zone. In particular, investigation on the crustal structure and the crustal thickness is the key to understanding the stressconcentration and strain accumulation process. Recent travel time inversion analyses have elucidated 3D velocity structures in
the whole areas in the Japanese Islands. However, very few studies have paid attention to velocity discontinuities due to thelimitation of spatial resolution. A receiver function analysis can extract velocity discontinuities at any depth. In this study, weapplied the grid search analysis of receiver functions to estimate the depths of Moho discontinuity beneath the Japanese Islands.
We first searched for the best-correlated velocity structure model between an observed receiver function at each station andsynthetic ones for 10 seconds from the direct P arrival. Synthetic receiver functions were calculated from many assumed onedimensional velocity structures that consist of a sediment layer and one or two velocity discontinuities from the ground surface
to the depths of 50 km. We considered only the positive S-wave velocity steps. Observed receiver functions were stacked without
considering backazimuth or epicentral distance. Telemetric seismographic network data covered on the Japanese Islands and several temporal dense seismographic stations are used. We selected events with magnitudes greater or equal to 5.0 and epicentral
distances between 30 and 90 degrees based on USGS catalogue.
As a result, we clarify spatial changes of the depths of Moho discontinuity. They tend to increase in mountain regions andbecome shallow toward the surrounding areas with some undulations in most part of the Japanese Islands. This grid searchanalysis extracts the oceanic Moho of subducting plates in some areas near the Pacific coastline and beneath the south westernJapan. This result suggests that velocity gaps of the subducting plates are larger than that of the overriding plate. We also show
the Itoigawa-Shizuoka Tectonic Line (ISTL) is the boundary of the velocity structure in the Japanese Islands. The uppermost
mantle along the ISTL shows relatively low P-wave velocities compared to the neighborhood areas. The southwestern Japanside is covered in the relatively high velocity and low Vp/Vs in the crust. On the other hand, the northeastern Japan side hasheterogeneities of velocity perturbations. Low S-wave velocity and high-Vp/Vs areas exist just beneath the Moho discontinuity.
This may be the reason the depths of Moho discontinuity interpreted from depth-converted receiver functions are deeper than theestimation from tomographic imaging and travel time of the refracted seismic waves in several areas.

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SCG57-P26

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Reassessment of the stress history in the eastern Boso Peninsula, central JapanYAMANAKA, Katsumasa1∗ ; SATO, Katsushi1 ; YAMAJI, Atsushi11Div. Earth Planet. Sci. Kyoto Univ.

There are numerous mesoscale faults in the Neogene to Quaternary Awa and Kazusa Groups in the earstern Boso Peninsula(Kinugasa et al., 1969). The counterclockwise change of the Philippine Sea plate motion was argued on the basis of the stresshistory reconstructed by fault striation analyses in the peninsula (Angelier and Huchon, 1987; Yamaji, 2000). However, there has
been no consensus on the timing of N-S or NE-SW compression. The timing was said to be about the late Pliocene by Kinugasa(1969), before 3-2 Ma by Angelier and Huchon (1987) and before 1.2 Ma by Yamaji (2000). In this research, we reinvestigated
the stress history by using a recent technique of paleostress analysis (the Hough-transform-based inversion method: Yamaji etal., 2006; Sato, 2006).
We investigated mesoscale faults cropping out along the east coast of the Boso Peninsula and collected about 1,400 fault-slip
data in the Awa and Kazusa Groups. The result of the fault striation analysis is as follows; a vertical axial compression, N-S
extension and NW-SE extension were detected from the upper Katsuura Formation to the Umegase Formation. In addition to theabove-mentioned three stresses, we detected NE-SW compression from the Amatu Formation to the Kurotaki unconformity andan early stage extension from the Amatsu and Kiyosumi Formations. The clarified stress history is summarized as follows; theearly stage extension before ˜3 Ma, the NE-SW compression at 3-2 Ma, the NW-SE extension at 2-0.8 Ma, the N-S extension
after 0.8 Ma and the vertical axial compression at the present.
The most important discovery of this study is that the compression was episodic from 3 to ˜2 Ma. In this presentation, we
discuss the relationship between the paleostress and the past position of the TTT junction.
Reference:
Angelier and Huchon, 1987, Earth and Planetary Science Letters, 81, 397-408.
Kinugasa et al., 1969, Bulletin of the Geological Survey of Japan, 20, 13-38 (in Japanese with English abstract).
Sato, 2006, Tectonophysics, 421, 319-330.
Yamaji, 2000, Journal of Structural Geology, 22, 429-440.
Yamaji et al., 2006, Journal of Structural Geology, 28, 980-990.
Keywords: Boso Peninsula, stress history, fault striation analysis

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SCG57-P27

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Analysis of fault rocks along Median Tectonic Line in Tsukide, Itaka town, Matsusaka
city, Mie prefecture
ARAI, Shun1∗ ; TAKESHITA, Toru1
1

Hokkaido University

Median Tectonic Line (MTL) is extended more than 800 km in the East-West direction in Southwest Japan, and it is the largest
fault, which defines the boundary between Sambagawa belt belonging to the Outer Zone of Southeast Japan and Ryoke belt
belonging to the Inner Zone of Southeast Japan. Cracks are initiated when the accumulated strain exceeds the strength of rocks,
and we call the displacement along cracks faulting, which could generate earthquakes. However, it is difficult to directly observe
presently occurring fault movement in the underground. Therefore, it is very important to observe the outcrop of faults, whichwere active in the past for understanding the development of fractures along faults. In this study, we described geological map
around the MTL, which is distributed in Tsukide, Iitaka town, Matsusaka-city, Mie-prefecture, and carried out rock descriptions.
Then, we showed brittle fracture formed by faulting along the MTL, and the development of geological structures related to thefaulting.
In this study, we mapped (i.e. investigated lithology) five valleys in high resolution using a 50 m scale, which extend approximately 150m in N-S direction, in the area spanning 900m in E-W direction, including the MTL. As a result of field study, it
has been found that the MTL dips north at high angles. We showed that around the MTL four kinds of rocks are structurally
overlain in order of the Sambagawa pelitic schist (50m+), pelitic schist derived from chert-laminite (90m), cataclasite (80m),
and protomylonite derived from Ryoke Granitoids (15m+). We sliced the cataclasite samples and the protomylonite ones, andobserved them under a microscope. Then, we observed the gradual alteration of plagioclase to muscovite, and chlorite depositedin cracks from the fluids which percolated along brittle fractures. We classified deformed granitic rock samples into four groups:
not fractured, weakly, moderately, and strongly fractured rocks based on the degree of cataclasis. The schistosities of Sambagawa
metamorphic rocks in the study area strike East-West directions, and the boundaries between Sambagawa metamorphic rocks
and Ryoke Granitoids are also traced in the East-West directions. Therefore, we can show that the MTL generally strikes theEast-West directions. Minor faults in Sambagawa metamorphic rocks strike NE-SW and dip north at moderate angles. Therefore, they are interpreted to be Riedel shears formed in relation to large-scale, left-lateral shear along the MTL in the East-Westdirection. Based on our detailed geological mapping in this area, it has been found that the trace of the MTL is displaced by
70m in the North-South direction in the center of this area, which could indicate a fault jog (step). Faults generally exhibit
non-monotonous structures (fault jog) such as bending, echelon arrangement, and junction. Fault jogs are the end areas or thestop areas of fracturing, and it is considered that there are asperities which indicates the area greatly slipped just adjacent to them(e.g. Sugiyama et al,. 2003). In the future study, we must investigate the structures of fault jog in detail. Further, we showedthat the rocks are strongly fractured near the MTL, and are moderately fractured far from the MTL. The degree of alteration ofplagioclase conforms to this result. From these results, it can be inferred that the fracturing along the MTL propagated from therocks in direct vicinity to the MTL to the remote ones, and the cataclasite zone grew over time.

Keywords: Median Tectonic Line, fault rock, cataclasite

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SCG57-P28

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Characteristics of island arc deformation due to steady plate subduction
FUKAHATA, Yukitoshi1∗ ; MATSU’URA, Mitsuhiro2
1

Disaster Prevention Research Institute, Kyoto University, 2 Institute of Statistical Mathematics

Steady plate subduction elastically brings about permanent lithospheric deformation in island arcs, though this effect has
been neglected in most studies based on dislocation theory. We investigate the characteristics of the permanent lithosphericdeformation using a kinematic model, in which steady slip motion is given along a plate interface in the elastic lithosphere
overlying the viscoelastic asthenosphere under gravity. As a rule of thumb, long-term lithospheric deformation can be understoodas a bending of an elastic plate floating on non-viscous fluid, because the asthenosphere behaves like water in a long term. The
steady slip below the lithosphere-asthenosphere boundary does not contribute to long-term lithospheric deformation. Hence, thekey parameters that control the lithospheric deformation are only the thickness of the lithosphere and the geometry of the plateinterface. Slip on a plate interface generally causes substantial vertical displacement, and the gravity always tries to retrieve theoriginal gravitational equilibrium. For a curved plate interface gravity causes upward bending of the island arc lithosphere, while
for a planar plate interface gravity causes downward bending. Larger curvature and thicker lithosphere generally causes larger
deformation. When the curvature changes along the plate interface, internal deformation is also involved intrinsically, which
modifies the deformation field due to gravity. Because the plate interface generally has some curvature, at least near the trench,
upward bending of the island arc lithosphere, which involves uplift of island arc and subsidence around the trench, is always
realized. On the other hand, the deformation field of the island arc lithosphere sensitively depends on lithospheric thickness
and plate interface geometry. These characteristics obtained by the numerical simulation are well consistent with observed
topography and free-air gravity anomalies in subduction zones, where a pair of topography and gravity anomaly, high in thearc and low around the trench, exists without exceptions all over the world, while there are large variety in the amplitude andhorizontal scale.
Keywords: island arc, crustal deformation, viscoelasticity, gravity anomaly

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SCG57-P29

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Structure of the PHS in the southernmost area of the Southern Japanese Alps using dense
seismic array records
KAWASAKI, Yusuke1∗ ; WATANABE, Toshiki2 ; KATO, Aitaro1 ; KANO, Ken-ichi3 ; ITO, Tanio4 ;ABE, Susumu5 ; NODA, Katsuya6 ; KOUCHI, Yoshinori6 ; YAMAOKA, Koshun1
1

Nagoya University, 2 University of Tokyo, 3 Shizuoka University, 4 Teikyo Heisei University, 5 JGI, Inc., 6 Geosys, Inc.

The southernmost area of the southern Japanese Alps is located within a focal region of the anticipated Tokai earthquake andat the western edge of the Izu collision zone. The structure of the subducting Philippine Sea Plate (PHS) in this area, however,remains enigmatic. To investigate the structure of the subducting PHS as well as the physical property of the oceanic crust, we
deployed a temporary, dense array consisting of 34 portable seismic stations extending 50 km in the southernmost area of thesouthern Japanese Alps. The seismic line started from Umegashima, Aoi-ku, Shizuoka city, and ended at Haruno-cho, Tenryuku, Hamamatsu city in Shizuoka prefecture. We applied receiver function and seismic tomography to the observed data, anddiscussed lateral variations of the plate interface and physical properties of the subducting oceanic crust in the studied area.
The analysis in this study is as follows.
1. We estimated velocity discontinuities by applying receiver function analysis to the seismic waveforms recorded by both thepresent array and five Hi-net stations near the array for teleseismic events with epicentral distance from 30 to 90 degrees.
2. We estimated seismic velocity structures by applying the double-difference tomography method (Zhang and Thurber, 2003)
to the arrival time data. We used seismic waveforms of 354 local earthquakes retrieved at both the seismic array deployed by thepresent study and permanent seismic stations (45 stations) around the array.
3. To investigate seismicity in the studied area, we relocated the earthquakes from January 2004 to October 2014 applying the
double-difference relocation (Waldhauser and Ellsworth, 2000) using the final velocity model estimated by seismic tomography.
We interpret the configuration of the PHS in the receiver function image. As overall character, the plate interface beneaththe seismic array gradually becomes shallow toward the northeastern side. The plate interface interpreted in the present study
well matches with those proposed by Matsu’ura et al. (1991), Kato et al. (2010), and Ito et al. (2013) at the both edges of thesection. For example, Hirose et al. (2008) delineated the smooth plate interface of the PHS. However, the interpretation in thisstudy suggests that the plate interface of the subducting PHS is not simply smooth, but has a convex, complex structure in thestudied region. Interestingly, this complex configuration well correlates with the spatial distributions of intraslab earthquakes.
A likely explanation is bucking deformation of the PHS due to the effect of collision and subduction. Subduction of a sea
mountain beneath the seismic line as seen in the southwest part of the studied area (e.g., Kodaira et al., 2004) is another possible
explanation. The reason is under discussion.
From the center to the southwestern side of our seismic section, oceanic crust is characterized by relatively low Vs with ahigh Vp/Vs ratio. The oceanic crust in this area does not host any significant seismicity. In contrast, at the northeastern sideof our seismic section, a low Vp/Vs ratio seems to be present within the oceanic crust, and hosts active seismicity therein. A
plausible explanation of the low Vp/Vs ratio within the oceanic crust is that intra-oceanic island arc crust is subducting beneaththe northeast side of our seismic section. We suggest that different amount of water trapped within the subducting oceanic
crust beneath the studied area may control lateral variations of activity level of non-volcanic tremors or deep low-frequency
earthquakes at down-dip extension.
Keywords: southernmost area of the southern Japanese Alps, Philippine Sea Plate, receiver function, seismic tomography, intraoceanic island arc crust, deep low-frequency earthquakes

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SCG57-P30

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Holocene vertical movement history in northern Sanriku coast, NE Japan, related tomegaquake cycle
KIKUCHI, Ryoichi1 ; MIYAUCHI, Takahiro2∗
1

Dept.Earth Sci., Fac. of Sci., Chiba University, 2 Dept.Earth Sci., Grad. School of Sci., Chiba University

The 2011 off the Pacific coast of Tohoku Earthquake (The 2011 EQ below) was associated with the distinct subsidence along
the Pacific Coast of NE Japan in addition to inter-seismic rapid subsidence by the asperity (coupling) of Eurasia (North American) plate and Pacific plate (Ozawa et al., 2011). Especially, the southern Sanriku coast which largely subsided has been reversely
uplifting as an after-slip movement, recovering one fourth of coseismic subsidence (GIS, 2014). If after-slip movement continues
at the same speed, the coast will start inter-seismic subsiding by the reinforcing interplate coupling after relatively short recoveryof coseismic subsidence (Ikeda, 2014). According this scenario, the vertical movement of northern Sanriku coast out of the 2011
EQ source area is possibly controlled by the similar megaquake cycle. We reconstructed the vertical movement history in thesouthern Sanriku coast based on the mapping of Holocene emerged coastal topographies and ages, and examined the megaquake
cycle managing the history considering the geodetic subsidence measured at the tide-gauge station.
Tephrochronologically age-determined MIS 5e marine terrace height of 30 m shows average uplift rate of 0.2 mm/yr in geological long term. Holocene emerged coastal topographies and dates present three times of rapid uplift events; about 1,000 years
ago just before B-Tm ash fall, before 3,300 years ago and before 4,800 years ago. Records of Hachinohe tide-gauge station in
the past 60 years indicate the mean subsidence rate of 2 mm/yr. We built the vertical movement diagram synthetically explaining
the above results.
Emergences of coastal topographies suggest three sudden uplift events which are named E1, E2 and E3 in chronological order.
Assuming that the geodetic subsidence (2 mm/yr) continued during 1,000 years between E3 and the present, E3 was associatedwith 6-7m uplift. Setting that the gradient of straight line connecting heights of emerged topographies attained just after uplift
events satisfies the long-term uplift rate of 0.2 mm/yr, E2 was accompanied by 5-6 m uplift 3,800 years ago, and E1 by 4-5 m
6,200 years ago. These abrupt uplift phenomena is likely generated by an near-shore faulting (Miyauchi, 2012), which is not
sufficiently testified by geophysical exploration yet. Correlating these uplift events with the ongoing after-slip uplift event after
2011 EQ, plate-boundary megaquakes associated with distinct coseismic subsidence necessarily occurred off the northern Sanriku coast, namely from the northern Japan Trench to the southern Kuril Trench, just before those uplift events. Such megaquakes
are estimated to occur at least three times in Holocene.

Keywords: Holocene, Emerged coastal topography, Vertical movement history, After-slip movement, northern Sanriku coast,
megaquake

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SCG57-P31

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Crust and upper mantle structure of the New Madrid Seismic Zone: Insight into intraplate
earthquakes
CHEN, Chuanxu1 ; ZHAO, Dapeng1∗ ; WU, Shiguo1
1

Tohoku University, Department of Geophysics

The New Madrid Seismic Zone (NMSZ) is seismically the most active region in the Central and Eastern United States and an
ideal area to study intraplate earthquakes. A sequence of at least three large earthquakes (M >7.0) occurred here in 1811-1812,and palaeo-seismic records show evidence of large earthquakes about 500 years apart in the past 2000 years. The distributionof local earthquakes recorded since 1974 delineates three linear faults in the NMSZ: (1) the NE-trending Cottonwood GroveBlytheville Arch fault along the central Reelfoot rift, (2) the NW-trending Reelfoot Fault, and (3) the NNE-trending New Madrid
North Fault. The activation of these mid-continental faults and their controls on duration of the seismic activity remain poorly
understood. One of the fundamental questions is: what makes the NMSZ different from the surrounding intraplate areas in North
America, especially the areas within the same geologic settings?
We determined a 3-D P-wave velocity model of the crust and upper mantle down to 400 km depth to investigate structural
heterogeneity and its influences on the generation of intraplate earthquakes in the NMSZ. We used 4871 high-quality arrival
times from 187 local earthquakes and 30,846 precise travel-time residuals from 1041 teleseismic events recorded by the EarthScope/USArray Transportable Array. Our results show that, beneath the Reelfoot rift, a significant low-velocity (low-V) zone
exists in the upper mantle down to 200 km depth, with a large volume of 200 km x 200 km x 150 km. The origin of the low-Vzone may be related to the passage of the Bermuda hotspot and the stalled ancient Farallon slab materials foundering in the
mantle transition zone. This low-V zone may have relatively low shear strength and act as a viscously weak zone embedded in
the lithosphere, being apt to concentrate tectonic stress and transfer stress to the seismogenic faults in the upper crust, leading to
the large intraplate earthquakes in the New Madrid Seismic Zone.
Keywords: New Madrid, earthquake, crust, mantle, velocity structure

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SCG57-P32

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The property of fault zone and fault activity of the Shionohira Fault, Fukushima Prefecture, JapanKAMETAKA, Masao1∗ ; SAKAI, Toru1 ; INADA, Noriyuki1 ; TANAKA, Yumiko1 ; OKAZAKI, Kazuhiko1 ;SUZUKI, Yuji1 ; AOKI, Kazuhiro2 ; TANAKA, Yoshihiro2 ; SESHIMO, Kazuyoshi2 ; NAKAYAMA, Kazuhiko2
1

Dia Consultants, 2 Japan Atomic Energy Agency

Co-seismic surface ruptures trending NNE-SSW direction were formed from Tabiuto-Nameishi to northwestern IshizumiTsunaki in Tabito-cho, Iwaki City, Fukushima Prefecture, by the April 11, 2011 Fukushima-ken Hamadori Earthquake. This
earthquake was characterized by the westward dipping normal slip faulting, and the maximum displacement was about 2 m (e.g.,
Kurosawa et al., 2012). These surface ruptures were newly named the Shionohira Fault by Ishiyama et al. (2011).
Before the 4.11 earthquake, the N-S trending several faults were described in this area as the Itozawa Fault in Active Faults
in Japan, New Edition (The Research Group for Active Faults of Japan, ed., 2011). The surface ruptures of 4.11 earthquake arecorresponding to a part of the Itozawa Fault (western trace of the Itozawa Fault by Tsutsumi and Toda, 2012). The geomorphological features of active faults were not found in the northward of the Gozaisyo highway. On the other hand, the N-S trending
lineament are recognized from the south of the Tabiuto-Nameishi to the boundary between the Fukushima and Ibaraki Prefectures, though surface ruptures did not appear in this area. The authors study the differences of active and non-active sections by
the 4.11 earthquake, and here the authors show the results of observation of fault outcrops along the Shionohira Fault.
A lot of new fault outcrops were formed by the 4.11 earthquake, however most of them are composed of foot-wall with fault
plane, and the structures of hanging-wall are difficult to observe. Only a few outcrops have basement rocks of the hanging-walland hoot-wall with fault plane. Three of these outcrops (Kyodo-gawa, Shionohira and Betto) were selected to investigation.
In addition, a fault outcrop (Nameishi-minami) located in about 300 m south to the southern tip of the surface ruptures wasinvestigated. We carried out observations of outcrops, polished slabs and thin sections, and X-ray diffraction (XRD) to the fault
materials.
As a result, the fault zones originated from schists were investigated at Kyodo-gawa and Betto. The thick fault gouge is cut by
a fault plane by 4.11 earthquake in each outcrops. The fault materials originated from schists are fault bounded with (possibly
Neogene) weakly deformed sandstone at Shionohira. The thin fault gouge is found along the fault plane by 4.11 earthquak.
A small-scale fault zone with thin fault gouge are observed in Nameishi-minami. According to XRD analysis, smectite was
detected in the gouges from Kyodo-gawa, Shionohira and Betto, while it was not contained in the gouge from Nameishi-minami.

References
Ishiyama, T., et al., 2011, Newsletter, Seismol. Soc. Japan, vol.23, no.5, 36-39.
Kurosawa, H., et al., 2012, Active Fault Res., no.36, 23-30.
The Research Group for Active Faults of Japan, ed., 2011, Active Faults in Japan, New Edition: Distribution map and therelated materials. Univ. Tokyo Press, 437p.
Tsutsumi, H. and Toda, S., 2012, Jour. Geol. Soc. Japan, vol.118, no.9, 559-570.

Keywords: Shionohira Fault, active fault, fault gouge, property of fault zone, X-ray diffraction, Fukushima-ken Hamadori Earthquake

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Deformation process of the Miocene Misaki assemblage at Cape Muroto, Shikoku, JapanTONAI, Satoshi1∗ ; MOURI, Keiji11Faculty of Science, Kochi University

We report the geologic structure of the Misaki assemblage, which constitutes part of the youngest portion of the Shimanto
accretionary complex, Shikoku, Japan. It is interesting to compare the deformation process of this strata with that of the present
Nankai accretioary complex. We divided the Misaki assemblage into ten lithofacies, and described lithologic map and geologic
cross section of the study area.
The northern part of the study area consists mainly of hemipelagic calcareous mudstone and deformed sandstone and mudstone.
In contrast, the southern part of the study area consists of folded turbidite and conglomerate. These strata dip to the west morethan 70o and are intruded by Miocene igneous rocks. Many minor faults are observed in the study area.
These lithologic and structural data suggests a deformation process of the Misaki assemblage as follows: (1) deposition ofocean plate stratigraphy, (2) offscraping by frontal thrusts, (3) intrusion of igneous rocks along one of the thrusts, and (4) tiltingof the whole strata.

Keywords: accretionary complex, Shimanto belt, Muroto, fault

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SCG57-P34

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Interseismic plastic deformations at ancient crustal seismogenic zones in the Hidaka metamorphic belt and Napier Complex
TOYOSHIMA, Tsuyoshi1∗
1

Niigata University

Pressure solution-precipitation structures are characteristically abundant in pseudotachylyte-producing fault zones in the Hidaka metamorphic belt, Hokkaido, northern Japan (Toyoshima et al., 2004; Wada et al., 2005). The zones occurred at thelowermost part of upper continental Hidaka crust. Pseudotachylytes formed under granulite-facies conditions (lower continental
crustal conditions) occur at Tonagh Island in the Napier Complex, Eastern Antarctica (Toyoshima et al., .1999). Seismic faulting(pseudotachylytes-producing faulting) and plastic deformation (formation of ultramylonite) alternated under lower continental
crustal conditions in Tonagh Island (Toyoshima et al., 1999). I illustrate interseismic deformations related to the Hidaka andTonagh pseudotachylytes as examples of ancient seismogenic zones in upper and lower crust, respectively.
Modes of occurrence of the Hidaka pseudotachylytes indicate that seimic slip with pseudotachylyte generation and slow plastic
deformation (pressure solution with precipitation) occurred alternatively and repeatedly in the same fault zones and fault surfaces(Wada and Toyoshima, 2006, 2007). Pressure solution-precipitation is likely one of the principal deformation mechanisms forinterseismic plastic deformation and time-dependent strength recovery of fault zones (Wada and Toyoshima, 2006, 2007). The
pressure solution-precipitation processes lead to increase in number of grain-to-grain contact and in real contact areas of the fault
surfaces, resulting in healing of the fault zones (Wada and Toyoshima, 2007). Very thin and sharp shear zones filled with veryfine-grained materials cut the pressure solution-precipitation structures and are cut by pseudotachylytes-producing faults. The
shear zones are deformation structures formed immediately before seismic faulting in the upper Hidaka crust.
Granulite-facies ultramylonites are characteristically abundant in and along the Tonagh pseudotachylyte-producing fault zones.
There are two different types of the granulite-facies ultramylonites in microstructures of recrystallized plagioclase grains: type 1
and 2. Type 1 ultramylonites have polygonal medium grains of plagioclase with smooth grain boundaries and very weakly undulose extinction. Type 2 ultramylonites include very fine grains and elongated fine grains of plagioclase with strongly undulose
extinction and irregular grain boundaries. Type 2 ultramylonites occur along granulite-facies pseudotachylytes-generating fault
surfaces and have been cut by fault veins of pseudotachylyte. Some of the granulite-facies pseudotachylytes became type 1 and 2
ultramylonites, which have also been cut by other granulite-facies pseudotachylytes. These may also be conspicuous difference
between dynamic recrystallization mechanisms of plagioclase immediately before and after seismic faulting.
Keywords: pseudotachylyte, pressure solution, ultramylonite, plastic deformation, interseismic deformation, time-dependent
strength recovery

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SCG57-P35

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Study on heterogeneous structure beneath the Beppu-Haneyama fault zone
KAMIZONO, Megumi1∗ ; MATSUMOTO, Satoshi2 ; NAKAMOTO, Manami2 ; MIYAZAKI, Masahiro1
1

Department of Earth and Planetary Sciences, Graduate School of Sciences, Kyushu University, 2 Institute of Seismology andVolcanology, Faculty of Sciences, Kyushu University
The Beppu-Haneyama fault zone is the active fault zone in Japan, running from the Beppu Bay to western part of Oita
prefecture. In the Beppu area, the seismogenic layer is thin (about 10km). Since the structure beneath this layer could affectthe thickness, we need to get acquaintance of subsurface structure. This study estimated the heterogeneous structure of this fault
zone from distribution of the reflectors based on seismological analysis.
We analyzed the data observed at seismic stations deployed by Kyushu and Kyoto Universities, NIED and JMA. For simplicity,
we assumed homogeneous velocity structure to analyze the observed data. Normal move-out (NMO) processing was applied todetect reflectors. Seismic section normal to the strike direction of the fault zone reveals that reflective zone of the depth about
25km, which could correspond to the Moho discontinuity. Since numerous reflected waves beneath the seismogenic zone weredetected. The distribution of the reflectors generating these reflected phase might relate to the thickness of the zone.
Keywords: Beppu-Haneyama fault zone, heterogeneous structure, reflector

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SCG57-P36

Room:Convention Hall

Time:May 27 18:15-19:30

Anomalous seismic wave intensity distribution in the Tokyo Metropolitan area.
PANAYOTOPOULOS, Yannis1∗ ; HIRATA, Naoshi1 ; SAKAI, Shin’ichi1 ; NAKAGAWA, Shigeki1 ;KASAHARA, Keiji2
1

Univ. Tokyo, ERI, 2 Assoc. Develop. Earthquake Prediction

The intensities of seismic waves observed at the dense seismic array of the Tokyo Metropolitan Seismic Observation network(MeSO-net) inside the Kanto basin, display unusual distribution patterns. In several occasions, the highest intensities are notobserved in the area above an earthquakes hypocenter but appear sifted more than 20 km away. In order to understand the sourceof this unusual intensity distribution pattern, it is crucial to understand how the waves attenuate before they reach the surface.
The attenuation of seismic waves along their path is represented by the t∗ attenuation operator that can be obtained by fitting theobserved seismic wave spectrum to a theoretical spectrum using an ω 2 model. In order to create a high quality dataset, only 1449
earthquakes that are recorded with intensity greater than 0 in the Japan Meteorological Agency (JMA) intensity scale are selectedfrom the JMA unified earthquake list from April 1st 2008 to October 2nd 2013. A grid search method is applied to determine
the t∗ values by matching the observed and theoretical spectra. The t∗ data where then inverted to estimate a 3D Q structure withgrid points set at a 10 km spacing. We implemented the 3D velocity model estimated by Nakagawa et al., 2012 and in addition
we set the initial Q values at 100 for the 0 km grids and to 400 for the grids below them. The obtained model suggests average Q
values of 50∼100 inside the Kanto basin. Furthermore, a low Q zone is observed in the area where the Philippine Sea plate meetsthe upper part of the Pacific sea plate. This area is located at approximately 40 km depth, beneath the north-east Tokyo and west
Chiba prefectures and is represented by Q values <300. Earthquakes occurring on the Pacific plate pass through this low Q area
inside the Philippine sea plate and are attenuated significantly. The estimated attenuation distribution at the MeSO-net station
for these earthquakes implementing our 3D Q model greatly coincides with the observed seismic wave intensity distribution.
Stations where our model predicts high attenuation display low intensity values whereas stations where our model predicts low
attenuation display high intensities. The implementation of our findings could help towards a better understanding of the damage
area of future earthquakes and mitigate the disaster of the affected areas.
Keywords: Attenuation, Tomography, MeSO-net

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