STT53-P01

Room:Convention Hall

Time:May 24 18:15-19:30

Hypocenter location in an inhomogeneous velocity structure with three-dimensional traveltime table
KATSUMATA, Akio1∗
1

Meteorological Research Institute, JMA

An inhomogeneous velocity structure has considerable effect on the accuracy of the earthquake locations in complicatedtectonic setting areas like the Japanese Islands. Calculation time is still one of the problems for hypocenter location in a threedimensional velocity structure. We show a evaluation of calculation time of event location in a three-dimensionally (3D) inhomogeneous velocity structure with lookup tables for each seismic station on the Japanese Islands.
We made 3D traveltime tables for each station to reflect the 3D velocity structure in the event location. The traveltime tables
were prepared beforehand for each station. Traveltimes for a station were calculated at grid points of three-dimensional coordinate with a ray-tracing method by Um and Thurber (1987). Traveltimes were calculated for blocks of (1 deg.)X(1 deg.)X(50km)
where events had been detected. The grid interval in the block was set depending on distance from the station. The number ofstations and blocks are 1,813 and about 250 thousand, and it took about one month of elapsed time on a 128-core cluster machine.
Hypocenter calculation times of 11,448 event locations in January, 2014 were compared for 1D traveltime table (1D-TT), 3D
traveltime table (3D-TT), and 3D ray-tracing method (3D-RT). Arrival times in the unified seismic catalogue in Japan were used.
The calculation time of one event was within one second for 1D-TT and 3D-TT with an ordinary workstation. The maximum
calculation time for 3D-TT was quick enough to be used in interactive processing. On the other hand, some of the calculation
time of 3D-RT were more than 10,000 seconds. The time of the 3D-TT was about 1,800 times shorter than that of 3D-RT as anaverage of logarithmic calculation times. The difference between 1D-TT and 3D-TT is four times as an average of logarithmic
calculation times.
An interpolated traveltime is different from that calculated with ray-tracing method at the grid point of the blocks in our
method. The difference was checked at every grid point in the blocks. The maximum differences of 82% blocks were less than
0.1 second. However, those of 0.01% of blocks exceeded one second. The large difference was usually caused by stepwise
traveltime variation due to ray-path scattering.
Hypocenter locations were compared among ray-tracing, three-dimensional traveltime table, and one-dimensional traveltime
table. Whereas the locations of 3D-TT of 98.3% events were close to that of 3D-RT than that of 1D-TT, 3D-TT locations werevery close to those of 1D-TT for some events. Many of those events are offshore events or inland events with small differences.
It is considered that the location difference were partly caused by the unstable condition in hypocenter location.
Acknowledgments.
We used seismic data from the National Research Institute for Earth Science and Disaster Prevention, Hokkaido University, Hirosaki University, Tohoku University, the University of Tokyo, Nagoya University, Kyoto University, Kochi University, Kyushu
University, Kagoshima University, the National Institute of Advanced Industrial Science and Technology, the Tokyo metropolitan government, the Shizuoka prefectural government, the Kanagawa prefectural government, the City of Yokohama, the Japan
Marine Science and Technology Center, and the Japan Meteorological Agency.

Keywords: hypocenter location, inhomogeneous velocity structure, three-dimensional travel time table

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STT53-P02

Room:Convention Hall

Time:May 24 18:15-19:30

Temporal change of transfer functions of seismic waves caused by an air-injection into
the underground.
HONJO, Taiki1 ; TSURUGA, Kayoko1∗ ; KASAHARA, Junzo2 ; YAMAOKA, Koshun3 ; IKUTA, Ryoya2 ;ITO, Kiyoshi4
1Tokyo University of Marine Science and Technology, 2 Faculty of Science, Shizuoka University, 3 Earthquake and Volcano
Research Center, Graduate School of Environmental Studies, Nagoya University, 4 Disaster Prevention Research Institute, Kyoto
University
The Summary for Policymakers (SPM) of the Working Group I contribution to the IPCC’s Fifth Assessment Report reported
that warming of the climate system was unequivocal and concentrations of greenhouse gases had increased. The SPM of theWorking Group III contribution to the AR5 recognized that Carbon Dioxide Capture and Storage (CCS) contributed to reduce
CO2 emission. Since CCS has a risk of CO2 leakage into the underground, it needs a monitoring of CO2 reservoirs continuously
for long term.
In this study we examined the temporal change in a transfer function of seismic waves by an air injection into the undergroundin order to monitor the geophysical structure. Previous study for CCS showed that the temporal changes during the injection in
Nagaoka City, Niigata Prefecture in 2003 about once a month.
This study researched effects to seismic waves caused by injecting air. We used ultra-stable seismic source called ACROSS forthe continuous monitoring. ACROSS had been developed by Kumazawa et al. (2000) at Nagoya University and Tono Geoscience
Center. ACROSS source accurately controls and transmits seismic or electromagnetic waves to the underground continuously. We
monitor a small change of geophysical structure of the underground by estimating the transfer function between the transmitted
waves and observed data. We conducted the experiment with ACROSS sources and about 30 geophones near the Nojima Fault in
Awaji Island from February to March in 2011. An amount of injected air was about 81 ton into the underground during 5 days.
We analyzed the transfer functions focusing on the temporal variations of the amplitude and frequency which may effectively
change corresponding to the changes in the underground structure. Source characteristics (in a unit of force (N)) was estimatedfrom geophone data set near the source and transfer functions (in a unit of m/N)were calculated by deconvolution between
observed displacement data and source function. We attempted to detect the temporal changes of transfer functions by comparing
the variations of amplitude and frequencies in a target travel-time window before and after the injection. We analyzed somearbitrary travel time windows, in which a particular seismic phase arrive from the particular range in the underground assuming
as an isochronal scattering shell, after first arrival of transfer function.
As a result, we found that spectral amplitude at the particular frequencies (e.g. 12Hz and 14Hz) increased over 300% after
a day from the start of the air injection at a few observation sites in the eastern side of the injection well. Since such temporalchanges were observed at several observation sites and seemed to move towards the up-dip direction site in the eastern area of
Mt. Odo, we considered that it might be caused by injected air movements.
Keywords: monitoring, ACROSS

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STT53-P03

Room:Convention Hall

Time:May 24 18:15-19:30

Sophistication of the cloud type microtremor observation system
SENNA, Shigeki1∗
1

NIED

We have been seeking an efficient way to maximize the potential of the microtremor methods for shallow surveys. It isconsideredthat a practical approach has been gained in the observation by the development of portable seismometers (Senna, 2006,2012) and by the finding of the full usability of the data obtainable by a miniature array (radius less than 1m), optionally
togetherwith a small irregular-shaped array (radius less than 10 m) consisting of three seismometers (Cho et al., 2013a).
As an efficient way to infer an S-wave velocity structure, we consider that a classical, simple profiling method (SPM), wherea dispersion curve is directly converted into an S-wave velocity structure (e.g., Heukelom and Foster, 1960), is a good schemefrom a view point of simplicity, thus, the balance between the efforts and the information to be extracted. It is true, however,that
we frequently like to increase to resolution. Facing this dilemma, we suggested a simple tool H/V depth conversion (Cho etal., 2013). We found that the use of an H/V depth conversion followed by a simplified inversion method (SIM) of Pelekis andAthanasopoulos (2011) can in fact increase the resolutions (e.g., Senna et al., 2013; Yoshida et al., 2013).
The current challenge is to further promote the efficiency in the data processing procedure. A visual reading of analysis results,
which we take at the current time, is time consuming to deal with a vast mount of microtremor data, now obtainable by astreamlined observational procedure. The reproducibility and biases depending on analyst constitute other kinds of problem ofvisual reading.
Keywords: microtremor, miniture array, cloud system, underground structure model, S-wave vlocity

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STT53-P04

Room:Convention Hall

Time:May 24 18:15-19:30

Construction of the seismic observation network around Shimokita Peninsula (2)NOGUCHI, Shinako1∗ ; SEKINE, Shutaro1 ; SAWADA, Yoshihiro1 ; KASAHARA, Keiji1 ; SASAKI, Shunji1 ;TAZAWA, Yoshihiro1 ; YAJIMA, Hiroshi1
1

Association for the Development of Earthquake Prediction

In Japan, dense seismic observation networks have been installed including high-sensitivity seismograph network (Hi-net)
operated by NIED. While these networks were relatively thin around northern Tohoku and southeastern Hokkaido. It decreased
the earthquake detection capability in this region compared to other regions. Under the circumstance, we installed high-sensitivity
seismic network (AS-net) in this region, Shimokita, Tsugaru and southeastern Hokkaido, and started real-time monitoring forearthquake activity (Sekine et al., 2014). In this presentation, we report the first fruits by AS-net system after the completion of
network installation and data release.
We have completed the installation of AS-net which consists of 36 observation sites at August 2014, in addition to 20 stations
already installed in 2013. Seismic data recorded by AS-net are distributed at the nation-wide real-time distribution network forseismic data, JDX-net. From January 2015, it became able to download the seismic data by AS-net via continuous seismic data
download web service managed by NIED. It would contribute to enhance the precision of seismic monitoring and any otherresearches for seismology.
We estimated the level of background noise for each AS-net station. As a noise level, we calculated the root-mean-square(RMS) value for the amplitude of 1 hour ambient noise waveform. As a result, the noise level in daytime exceeds 50 micro-cm/s
at 11 stations. On the other hand, the noise level in daytime was around 10 micro-cm/s or less at 14 stations. At the stations
with higher noise level, the ambient noise were dominant at 0.5-1 Hz. The measured average S-wave velocity (Vs) for soil layer
between the seismometer at borehole bottom (˜20 m depth) and ground surface was related to the noise level for each station; thestations with averaged Vs of 300 m/s or less tended to show higher noise level. It indicates that the noise level at each station
depends on the soil condition.
Then we relocated earthquakes around Shimokita region during 2014 automatically using AS-net data in addition to the otherstations nearby. Up to 4616 events were determined by our relocation, which are 2.5 times as many as JMA hypocenter catalogue(1846 events). Of course, our result contains some artificial events; blasts, seismic exploration and so on. For natural earthquake,we caught 375 events during a swarm around Towada from 20 to 31 January 2014 (287 events in JMA catalogue). To distinguishthese various events we got, we will check them in detail with manual measurement. Frequency-magnitude diagram for ourcatalogue peaks out at around M0.6 while that for JMA catalogue peaks out at around M1. It implies that the AS-net enhanced
earthquake detection capability around Shimokita region.
Reference;
Sekine, S., S. Sawada, K. Kasahara, S. Sasaki, Y. Tazawa, H. Yajima, 2014, Construction of the seismic observation network
around Shimokita Peninsula, Jaman Geoscience Union Meeting 2014, Yokohama, STT57-P09, April 2014.
Keywords: Seismic observation network, Shimokita Peninsula

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STT53-P05

Room:Convention Hall

Time:May 24 18:15-19:30

Azimuth verification of the MeSO-net accelerographs: towards the imaging of groundmotions in the Kanto area
KANO, Masayuki1∗ ; NAGAO, Hiromichi1 ; SHIOMI, Katsuhiko2 ; SAKAI, Shin’ichi1 ; NAKAGAWA, Shigeki1 ;MIZUSAKO, Sadanobu1 ; HORI, Muneo1 ; HIRATA, Naoshi1
1

ERI, the University of Tokyo, 2 NIEDIn the Tokyo metropolitan area of Japan, large plate boundary earthquakes repeatedly occurred with intervals ranging from 200
to 400 years in the case of M 8 class, and with an interval of approximately 27.5 years in the case of M 7 class. Rapid predictionof damages on constructions due to such a large earthquake is important to quickly decide the priority order in recovery actions
without waiting for on-site reports. Such a rapid prediction system requires an image of ground motion in the target area asan input, which is to be estimated from seismograms of dense seismological observation networks. A dense seismic arraycalled MeSO-net (Metropolitan Seismic Observation network), in which 296 accelerometers are installed with several kilometerintervals, was established in 2007 for the purpose of the disaster mitigation for forthcoming large earthquakes. Whether the actual
azimuths of MeSO-net seismometers newly installed after 2009 were really in the magnetic north or not have not been verified
yet, while the azimuths of three of the seismometers installed before 2008 were already confirmed to be in the opposite direction.
Since such obvious errors in the azimuths badly affect subsequent data processing, we evaluate the azimuths of all seismometers
based on the cross-correlation with seismograms recorded at nearby Hi-net tiltmeters and F-net broadband seismometers. Our
result suggest that the northward components at more than 80 % of stations are determined to be within 10 degrees from themagnetic north, while those at the three stations are reconfirmed to rotate more than 90 degrees as the previous study pointed out.
Keywords: MeSO-net, sensor azimuth, cross correlation, Hi-net, F-net

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STT53-P06

Room:Convention Hall

Time:May 24 18:15-19:30

Difference of availability between the F-net and the Hi-net seismograph networks before
the 2011 Tohoku earthquake
SUE, Yoshiki1∗
1

No institution affiliation

1. Introduction
It was reported that number of missing waveform images of the F-net, the broadband seismograph network of NIED, increased
before the subject earthquake (Sue, 2013).
With the aid of a document of the Headquarters for Earthquake Research Promotion, where availability of the F-net and theHi-net, high sensitivity seismograph network are shown, we do further investigation.
2. Investigation results
Fig.1 shows availability of the F-net and the Hi-net from April 2009 to March 2012. It shows the following phenomena.
- During the period of longer than 1.5 years from April 2009 to November 2010, availability of the F-net was close to 100%,though it became worse a little several times.
- Starting from December 2010, it became worse continuously, and it took minimum value in January 2011.
- Then it recovered, but it was worse than normal value.
- From February 2011, availability became worse again, and it took minimum value again.
- Then it recovered, though it was worse than normal values, and the 3.11 earthquake occured.
- It returned to normal state in May 2011.
- Availability of the Hi-net was almost constant, except for the days and one month after of the earthquake.
3. Issues
The following points to be discussed.
- For the duration of longer than 1.5 years, high availability of the F-net has been achieved. Why did it become worse startingfrom around 3 months before the 3.11 earthquake?
- Why did availability vary up and down during the worse period?
- Why was there difference in stability between the F-net and the Hi-net at the 3.11 earthquake?
4. Discussion
For several months before the earthquake of magnitude = 9.0, it is believed that the F-net seismographs had been affected insome way by the crust at their locations. Difference in stability between the F-net and the Hi-net could be because of differencein natural period of the seismographs. Natural period of the F-net seismograph is 360 seconds (STS-1 type) and 120 seconds(STS-2 type), whereas that of the Hi-net is 1 seconds. There were some sort of movements before the earthquake, which wererelatively slow. Thus only the F-net seismographs were affected.
The major cause for long-lasting trouble of the F-net is ”electric power supply trouble” according to the official information of
the F-net.
Gratitude: We thank NIED for the use of data for the F-net and the Hi-net.
References:
Yoshiki Sue, 2013, The increase in missing waveform images of the F-net broadband seismograph network preceding the 2011
Tohoku earthquake, JpGU2013 SSS30 P01.
Headquarters for Earthquake Research Promotion, 2013, 62nd Policy committee Survey observation planning unit meeting,62-(5) Seismograph networks of National Research Institute for Earth Science and Disaster Prevention (NIED).
http://www.jishin.go.jp/main/seisaku/hokoku13k/k62-5.pdf

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STT53-P06

Room:Convention Hall

Time:May 24 18:15-19:30

Caption of figure
Fig.1 Availability of the F-net(green) and Hi-net(red) Source: NIED
Availability of the F-net shows deterioration continuously from around 3 months before to after the 2011 Tohoku earthquake.
While that of the Hi-net does not show such a change.
Keywords: F-net, Hi-net, Seismograph, Availability, Seismograph network

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STT53-P07

Room:Convention Hall

Time:May 24 18:15-19:30

Characteristic evaluation of the most suitable seismic exploration array to detect a seafloor
topography change
TACHIBANA, Toi1∗ ; TSURUGA, Kayoko2
1

Graduate School, Tokyo University of Marine Science and Technology, 2 Tokyo University of Marine Science and Technology

Generally typical large-scale seismic exploration is not so suitable for isolated, small-scale areas. We expect that a marine
exploration with AUV (Autonomous Underwater Vehicles) can solve this problem because of its portability. In order to obtain
the dense and high-quality data, various exploration sources may require new type receivers array design.
In this study we therefore assessed the characteristics of survey design for optimum seismic exploration for a target near/undera sea-bottom by using an elastic wave simulation with an elastic finite-difference method (Larsen, 2000). We assumed that asurvey target was a stair-casing transformation at the sea bottom as long as 6 m. The model space was 1000m long and, 300m
long in horizontal and vertical directions, respectively, and water depth was 150m. The model space was divided into 0.2m-0.2m
staggered grids. We gave the parameter of P and S wave velocities (Vp, Vs), attenuation factor (Qp, Qs), and density (ρ). We
used a Ricker wavelet as a source time function with a central frequency of 100Hz and 50 receivers installed on the single receivercable. We calculated 54 cases of seismic records using 6 fixed sources and 9 receivers arrays. We found two important seismicphases, that is, secondary P-waves (called X-phase) and S-waves (Y-phase) that were excited by the target as a secondary sourcein order to detect the changes of bathometry and understructure. The X-phases were observed in all cases of receiver arrays, but
the amplitudes were small and they may be lost in background noises. The Y-phases had larger amplitudes than X-phase but
could not be observed by the undersea receiver. In a case of X-phase, the amplitudes became larger when the source was locatedat a lower area of the bathometry than that at a high area. In the case of X-phase, the largest amplitude was excited by the sea
bottom receivers array which was 4˜20 times as large as the other X-phases. In the case of Y-phase, the largest amplitude wasobserved at the receivers array at the sea bottom. We found that since the source on the sea bottom had the largest amplitude, it
was good to obtained high-quality data. It however noticed that an interval between the target and the source is required to be aappropriate distance not to overlap the secondary waves and the primary waves each other.
The location of bathometry change point in horizontal can be detected easily by using the seismic records of the X and the Yphases. But S/N ratio might be smaller because the amplitude of the X-phase and the Y-phase are small. Vertical array is divided
into the marine part and the underground part, so it can observe larger amplitude of those phases simultaneously. A vertical arrayis good to detect the bathometry change in the vertical direction and to obtain a high S/N ratio when the secondary waves andboundary waves with large amplitude can be observed. It however notices that this type of vertical array needs a high cost of theinstalling and the difficulty of the transport.
In summary, I suggest a seismic exploration array that has both a horizontal array and a vertical array. First, by using a towing
horizontal receivers array, the target location can be identified in a horizontal direction in a large area and then by using thevertical array to explore in detail. Before installing the vertical array, we suggest the use of AUV shoots near the sea bottom
because it can excite the large amplitude by boundary waves that can record X-phase more correctly. The vertical array is
expected to be installed at the upper side of the staircase at 100m away from the target. To observe the records with a higher
S/N ratio and to identify the location of the bathometry change in vertical direction. In future, there is an issue to calculate thegeometry and size of bathometry change by using the characteristics of frequency dependency.
Keywords: geophysical exploration, seafloor topography change, exploration array evaluation

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STT53-P08

Room:Convention Hall

Time:May 24 18:15-19:30

Broadband Seismic Array in Micronesia Zone, the South Western Pacific Region
ISHIHARA, Yasushi1∗ ; TANAKA, Satoru1 ; SUETSUGU, Daisuke1 ; OBAYASHI, Masayuki1 ;TONEGAWA, Takashi1
1

JAMSTEC

Although seismic network is well developed in continental and island arc region recently, oceanic region has still very sparse
seismic network. For further research of ocean plate, its substructure and geodynamic in the ocean region, seismic network in
the ocean are required. OHP/Pacific21 network is focusing Micronesia, the south western Pacific region. In this region only
some OHP/Pacific21 stations and USGS stations are under operation and still sparse network. JAMSTEC and ERI, Univ. ofTokyo have started to deploy Broadband Ocean Bottom Seismic (BBOBS) array for about two years around Ontong-Java Plateau
where is dynamic evidence of Earth’s history. Micronesia islands locate north edge of Ontong-Java Plateau. Then our group has
installed some seismic stations in Micronesia islands to place complement of BBOBS network.
In this program, we performed three items as follows, (1) Restart of measurement in Majuro, Marshall islands (2) Installationin Chuuk island and Kosrae island, FSM (3)Relocation of Palau station. Majuro station had long interval of measurement due topermission of land usage. We restarted observation in small island on Majuro atoll after negotiation. Fortunately this site is very
silent because this site is out of place of residence. Chuuk and Kosrae stations are installed as temporal stations jointing BBOBS
array supported by local residence. Last Palau station located in downtown, so that measurement condition was not fine. We
relocated new site where is silent filed area.
All stations listed above are off-line recording. Our group retrieves data on site about every six month. To reduce the risk ofdata gap by power supply trouble, line trouble, GPS trouble and system trouble, we installed observation system multiply for allparts.
As for new temporal stations, Chuuk and Kosrae stations, we retrieved the data last December. We evaluated noise signal
level and checked seismic event data. Generally seismic station is ocean island has high noise level and unstable recording. In
these new stations, both stations record stable data and low noise signal except oceanic wave origin’s signal. Especially horizontal
component of Chuuk station is close to low noise model in long period component. PKP phase excited by distant deep earthquake
is recorded in original raw data. The performance of these stations expects more fine quality data in long-term operation to our
research.

Keywords: Broadband seismic observation, Ontong-Java Plataeu

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STT53-P09

Room:Convention Hall

Time:May 24 18:15-19:30

Use of fuel cell system as a power source for seismic observation
KANO, Yasuyuki1∗ ; YOSHIMURA, Ryokei1 ; KATAO, Hiroshi1 ; MAEDA, Kensaku2 ; YAMASHITA, Masahiro2
1

Disaster Prevention Research Institute, Kyoto University, 2 TOYOBO CO., LTD.

Observation of earthquake or crustal deformation often deployed at sites where commercial power supply is not available. For
example, temporal observation after large earthquakes or observation area that is not covered by existing observation network.
Even at the site with commercial power supply, backup of power supply is essential in preparation for power cut caused bydisasters. In order to acquire continuous data before and after a large earthquake is
Battery or solar cell have been used for observations at the site where commercial power supply is not available. Batteries
are usually heavy and unsuitable for transportation. Solar cells cannot produce power during cloudy or rainy weather and night.
Although observation system with smaller power have been developed, a certain amount of power is still needed for particularsensors and telemetry.
Fuel cell systems that can be used for seismic and crustal deformation observation is recently developed. Fuel cell systems
stably supply power for long time. We made seismic observation at the Yagi observatory (DP.YGI) using a fuel cell system
as power supply to test feasibility of the fuel cell system. The system consists of a seismimoter, data logger (LS-7000XT,
Hakusan Corporation), fuel cell (TOYOBO ProtonCube(R)), solar cell, power controller, and mobile router (MR03LN, NEC
Platforms). The observation was began from December, 2014. The observation system satisfactorily operates in spite of poor
power production of solar cell because of snow and bad weather. The fuel cell equipped with two fuel tank of 10L, which cancontinue the observation for a half year. Increase of number of the fuel tank extends the observation period without exchange ofthe tank. We have plan to make test observations using the fuel cell system at other sites sensors and with different sensors.

Keywords: fuel cell, seismic observation, crustal deformation observation, temporal observation, power supply

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