Intrinsic and Scattering Seismic Attenuation in Southwestern Anatolia

Şahin, Şakir; Erduran, Murat; Alptekin, Ömer; Çakır, Özcan

doi:10.1007/s00024-007-0263-y

Cited by 11 publications

(2 citation statements)

References 35 publications

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“…In the 2 4 Hz band, scattering is strong in Hokkaido and northern Honshu, but it is weak in western Japan, and especially weak in Shikoku. 1 Kanto-Tokai, Japan (Fehler et al 1992), 2 Long Valley, California (Mayeda et al 1992), 3 Central California (Mayeda et al 1992), 4 Hawaii (Mayeda et al 1992), 5 Japan (Hoshiba 1993), 6 Southern California (Jin et al 1994), 7 Northern Greece (Hatzidimitriou 1994), 8 Southern Spain, < 170 km (Akinci et al 1995), 9 Southern California (Adams and Abercrombie 1998), 10 Northeastern Venezuela (Ugalde et al 1998), 11 Eastern Turkey (Akinci andEyidogan 2000), 12 Southern Apennines Bianco et al (2002), 13 South Central Alaska (Dutta et al 2004), 14 Southern Netherlands (Goutbeek et al 2004), 15 Northeastern Colombia (Vargas et al 2004), 16 Northeastern Italy (Bianco et al 2005), 17 Southern Sicily (Giampiccolo et al 2006), 18 Southern Anatolia (Sahin et al 2007), 19 Japan (average) (Carcolé and Sato 2010), 20 Southern central Andes (D <40 km) (Badi et al 2009), 21 Southern central Andes (40 km < D < 210 km) (Badi et al 2009), 22 Southeastern South Korea (Lee et al 2010) In the 8 16 Hz band, scattering is strong in Honshu; however, it is weak in Shikoku.…”

Section: Mltwa In Japanmentioning

confidence: 99%

Seismic Wave Propagation and Scattering in the Heterogeneous Earth : Second Edition

Sato¹,

Fehler²,

Maeda³

2012

452

385

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Scattering due to randomly distributed small-scale heterogeneities in the earth significantly changes seismic waveforms of local earthquakes especially for short periods. Scattering excites long lasting coda waves after the direct arrival and broadens the apparent duration of oscillation with increasing travel distance much longer than the source duration time. Models of propagation through deterministic structures such as those with horizontally uniform velocity layers cannot explain those observed phenomena. Our goal in writing this book is to put a focus on the phenomena of seismic wave scattering by distributed heterogeneities in the earth, especially in the lithosphere, where stochastic treatment is essential to describe both heterogeneous media and wave propagation through them. Stochastic approaches and deterministic approaches are complementary for the construction of a unified image of the earth's structure.Keiiti Aki was a distinguished pioneer who extensively developed various stochastic methods for short-period seismology. His strong encouragement and continuous support for us were essential in motivating us to write the first edition of this book. Before Kei passed away in 2005, he kindly cited our book when he argued for the importance of the study on seismic wave scattering caused by small-scale heterogeneity in his letter to V. I. Keilis-Borok, ". . . To a geodynamicist, the earth's property is smoothly varying within bodies bounded by large-scale interfaces. Most seismologists also belong to this "smooth earth club," because once you start with an initial model of smooth earth your data usually do not require the addition of smallscale heterogeneity to your initial model. As summarized well in a recent book by Sato and Fehler (1998), the acceptance of coda waves in the data set is needed for the acceptance of small-scale seismic heterogeneity of the lithosphere. There are an increasing number of seismologists who accept it, forming the "rough earth club." I believe that you are also a member of the rough earth club, judging from the emphasis on the hierarchical heterogeneity of the lithosphere. . . . "(Aki 2009).The first edition of this book was fortunately accepted in the geophysical community as a textbook, especially for graduate students. Furthermore it has been often cited in the physics community since this book introduced various aspects of wave scattering in real heterogeneous media. During the decade following the vii viii Preface to the Second Edition publication of the first edition, there were developments in stochastic methods and analyses focusing on seismogram envelopes. Radiative transfer theory has been used not only for the study of coda envelopes but also for the analysis of whole seismogram envelopes. These studies made it possible to resolve the spatial variation of scattering strength. There have been developments in the statistical description of wave propagation in random media that reliably predict the delay of peak amplitude from the onset and the broadening of seismogr...

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Section: Mltwa In Japanmentioning

confidence: 99%

Seismic Wave Propagation and Scattering in the Heterogeneous Earth : Second Edition

Sato¹,

Fehler²,

Maeda³

2012

452

385

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“…The attenuation properties of the east Anatolian plate boundary are similar to those in the other side of Anatolia. In western and southwest Anatolia, numerous studies have been carried out to found out the attenuation of seismic waves in the crust (AKıNCı et al, 1994;HORASAN and BOZTEPE-GÜ NEY, 2004;SAHIN et al, 2007;SAHIN, 2008). These studies have generally found out low values of Q c for tectonically and seismically active regions.…”

Section: Introductionmentioning

confidence: 99%

Estimation of Coda Wave Attenuation in the East Anatolia Fault Zone, Turkey

Sertçelik

2011

Pure Appl. Geophys.

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In this study, the attenuation of coda waves Q c (f) has been estimated for different lapse times and frequencies in the East Anatolia Fault Zone (EAFZ) in Turkey using a single back-scattering model of S-coda envelopes. The data include 255 earthquakes recorded by ten stations. The frequency-dependent Q c values are estimated at central frequencies of 1.5, 3, 6, 8, 12, and 18 Hz using 20-30-40 s lapse time windows. Along this fault zone, the frequency-dependent Q c obtained for all data and lapse time is Q c = 57.5f 0.82 . The entire study area is divided into six subregions according to the magnitude of the earthquakes and the location of the fault segments. The estimated average frequency-dependent relation for all lapse times are; Q c I ð Þ ¼ 34:3f 0:93 for Bingöl-KarliovaErzincan triple junction; Q c II ð Þ ¼ 56:3f 0:71 for Bingol-Lake Hazar segment; Q c III ð Þ ¼ 68:5f 0:75 for Lake Hazar-Sincik segment; Q c IV ð Þ ¼ 72:5f 0:78 Hazar-Sincik and Ç elikhan-Gölbaşı faults; Q c V ð Þ ¼ 59:7f 0:87 for Kahramanmaras triple junction and Q c VI ð Þ ¼ 67:4f 0:94 for Amanos Range and Karasu Basin. The lowest Q c is determined between Bingol and Malatya. The highest Q c value is along Amanos Range. In addition, Q c values are calculated for each regions at different lapse times. The average Q c value of the study region varies from 53 ± 11 at 1.5 Hz to 498 ± 41 at 18 Hz for 20 s lapse time window, as its variation is from 116 ± 11 at 1.5 Hz to 749 ± 75 at 18 Hz of central frequency for 40 s lapse time window. The increase of Q c with lapse times changes from one subregion to another along the fault zone. The rate of increment is significantly higher in Bingöl-Karliova-Erzincan triple junction than in the other subregions. This rapid increase of low Q c values in the junction reaches the general attenuation characteristics of the fault at 40 s lapse time. Finally, the low Q 0 and high n values can be attributed to the energy loss as a result of the heterogeneity and activity along the fault zone. The increase of Q c with frequency, lapse time may be related to heterogeneity decreases with depth. The rapid increase of Q c with depth in Bingöl-Karliova-Erzincan triple junction may be interpreted that the effect of the Northern Anatolian Fault Zone is effective in the upper crust is not so deep compared to EAFZ.

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