ライフサイエンスコーパス: seismic

1 d applications, including prediction of deep seismic activity and immobilization of nuclear waste in

2 ses and that, despite low deformation rates, seismic activity in the zone is not decaying with time.

3 Seismic activity increased even while injection rates de

4 Extensive seismic activity preceding the eruption shows that infla

5 Here, I review recent seismic activity that may be associated with industrial

6 This seismic activity was dominated by earthquakes associated

7 Seismic activity was highly unevenly distributed over ti

8 ly with only two days of detected precursory seismic activity.

9 ons, and high-intensity acoustic inputs from seismic airgun arrays or natural sources (e.g., earthqua

10 We demonstrate that a seismic analysis of stars in their earliest evolutionary

11 a receptor organ sensitive to low-frequency seismic and auditory stimuli.

12 Either possibility may explain the seismic and electrical anomalies that extend to a depth

13 alternative interpretation for the origin of seismic and geochemical anomalies in the deep lower mant

14 Seismic and geodetic observations in subduction zone for

15 for considering many optical devices in the seismic and geophysical context.

16 across the spin transition can help explain seismic and mineralogical models of the lower-mantle inc

17 generated strong tremor that was recorded by seismic and remote low-frequency acoustic (infrasound) s

18 he typical pattern and broadly expanding the seismic and tsunami hazard.

19 to convection, intensifying fronts, and even seismic and volcanic events.

20 ut forward to explain the measured pressure, seismic, and surface deformation behavior.

21 n believed to be one potential source of the seismic anisotropic layer at the bottom of the lower man

22 Shear wave splitting measures seismic anisotropy and is traditionally used to infer ch

23 upper mantle to predict the structure of the seismic anisotropy beneath ocean basins.

24 the lower mantle that reconcile the observed seismic anisotropy beneath the Tonga slab (V(SH)>V(SV))

25 sing the Global Positioning System (GPS) and seismic anisotropy data.

26 Seismic anisotropy from Rayleigh waves sampled at 15 s,

27 that phase H can be a source of significant seismic anisotropy in the lower mantle.

28 lived geochemical reservoirs and the lack of seismic anisotropy in the majority of the lower mantle e

29 The seismic anisotropy observations constrain the shape of t

30 nes, however, where regional observations of seismic anisotropy suggest that the direction of mantle

31 this anisotropy and show how an analysis of seismic anisotropy that incorporates measured ray path g

32 as the D'' reflector and the high degree of seismic anisotropy within the D'' layer.

33 arth's mantle-known as D''-shows significant seismic anisotropy, the variation of seismic wave speed

34 w field is consistent with observations from seismic anisotropy.

35 lso provides a strong mechanism for creating seismic anomalies in the inner core itself, much stronge

36 the robustness and distribution of positive seismic anomalies, inferred as subducted slabs, we creat

37 uring the 2011 typhoon season, we deployed a seismic array along the Chishan River in the mountain ar

38 We use seismic array analysis to illuminate the seismogenic roo

39 ismic P-to-S conversions recorded by a dense seismic array in North America.

40 se data recorded by the WOMBAT transportable seismic array to constrain a detailed (20 km resolution

41 ted spatiotemporal resolutions because dense seismic arrays are rarely sufficiently affordable for su

42 ecommunication fiber-optic cables into dense seismic arrays that are cost effective.

43 ults in the vicinity of the brittle-ductile (seismic-aseismic) transition.

44 g to weak interaction regimes in a system of seismic asperities embedded in a ductile fault zone matr

45 dary is parallel to the top of the plate and seismic attributes indicate a P-wave speed decrease of a

46 hese data provide insight into the long-term seismic behavior of the Loma Blanca fault and, by infere

47 Seismic body waves also intermittently detect a sharp ve

48 Here, we analyze the Japan seismic catalog in natural time from January 1, 1984 to

49 Here we investigate how the seismic characteristics of arc crust are transformed int

50 pe composition of calcite formed during this seismic cluster records rapid degassing of CO2, suggesti

51 Based on waveform modeling of seismic compressional waves that are reflected off the E

52 We show that the expected seismic contrast between the deformed perovskite-plus-po

53 to the development of physical models of the seismic cycle with potentially predictive power.

54 Drill cores and seismic data acquired during two cruises (SHALDRIL I and

55 the mantle is severely hampered by a lack of seismic data collected in marine areas.

56 Here, using seismic data combined with thermal models, we show that

57 Here we compile seismic data from subduction zone forearcs exhibiting re

58 Although well- and seismic data have established a 20 km thick stratigraphy

59 e available geomorphological, geological and seismic data in the literatures show that this model is

60 ls poking through shallow gas pockets in 3-D seismic data of the CNS indicating that about one-third

61 ic analysis of this doublet, we use regional seismic data providing robust two-point source models, f

62 e sensing and analyses of limited Apollo-era seismic data, deficiencies remain in our understanding o

63 ower-mantle bridgmanite is required to match seismic data, implying the presence of metallic iron in

64 Here using, high-resolution active-source seismic data, we show that Mount St Helens sits atop a s

65 l also makes a testable prediction of a post-seismic decrease of seismic velocity in the shallow crus

66 nSAR data processing results from early post-seismic deformation.

67 uation domain controls the largest monitored seismic, deformation, and geochemical unrest at the cald

68 ies in the drill core coincide with regional seismic discontinuities and reflect transient expansion

69 inverse scattering of SS waves the depths to seismic discontinuities below the Central Pacific, which

70 does not contribute significantly to global seismic discontinuities in the lower mantle.

71 The origin of a seismic discontinuity associated with this interface, kn

72 by residual upper mantle, producing a sharp seismic discontinuity at depths of around 38 to 42 kilom

73 We present a novel record of near-field co-seismic displacement, measured with 1-second temporal re

74 for the presence of reflected and converted seismic energy from the core.

75 kilometers per second, suggesting efficient seismic energy generation.

76 eismic P wave recordings indicate a radiated seismic energy of ~1.5 x 10(17) joules.

77 ent with transient effects of impact-induced seismic energy.

78 ions with nuclear yields being comparable to seismic estimates.

79 lation methods that reproduce both realistic seismic events and long-term earthquake sequences.

80 ur results suggest that detection of abiotic seismic events are biologically relevant and widespread

81 fective in the lower and middle crust, where seismic events are rare and resolution is generally poor

82 ded seismicity, providing evidence that some seismic events are related to magma intrusion.

83 The 13 distinct seismic events delineated by this effort demonstrate tha

84 The location of impulsive seismic events indicative of lava reaching the seafloor

85 of glacial earthquakes, globally detectable seismic events whose proper interpretation will allow re

86 earthquakes requires signals for forecasting seismic events.

87 Earth's inner core boundary, here we present seismic evidence for a localized 4-8 km thick zone acros

88 as been hypothesized several decades ago, no seismic evidence has ever been reported.

89 Here, we present bathymetric and seismic evidence showing that the caldera was not open t

90 Here we compare experimental and seismic evidence to test whether patterns of seismicity

91 egration of unique micropalaeontological and seismic evidence.

92 However, for seismic excitation, where energy is mostly carried by su

93 h scales, ranging from thermal vibrations to seismic excitation.

94 eismic body wave images from dense broadband seismic experiments that show higher than expected volum

95 graphic model, derived from on- and offshore seismic experiments, that reveals a strong low-velocity

96 Seismic exploration of Earth's deep interior suggests, h

97 f physiological disruption, we conclude that seismic exposure can harm scallops.

98 which slow slip has been reported, including seismic faults.

99 s observation has implications for enigmatic seismic features beyond ~2000 kilometers depth and sugge

100 rovide an explanation for the many enigmatic seismic features that are observed in ULVZs.

101 of advanced FWI methods to three-dimensional seismic field data.

102 ound motion prediction that uses the ambient seismic field.

103 e for some useful purpose, such as long-term seismic forecasting.

104 ximately 550 ka-the longest direct record of seismic frequency documented for any fault to date.

105 zone in northern Chile is a well-identified seismic gap that last ruptured in 1877.

106 The seismic gap theory identifies regions of elevated hazard

107 2014 a M 8.2 earthquake occurred within this seismic gap.

108 l concepts using examples from probabilistic seismic hazard analysis.

109 t for assessing fault displacement, defining seismic hazard and for predicting ground motion.

110 ve important implications for assessments of seismic hazard and our understanding of how faults inter

111 , they have been excluded from probabilistic seismic hazard assessment and aftershock hazard notices.

112 deling of realistic slip profiles for use in seismic hazard assessment and paleoseismology studies.

113 ly understood, and our ability to assess the seismic hazard associated with geothermal energy or unco

114 Seismic hazard in continental rifts varies as a function

115 uld motivate reevaluation of these issues in seismic hazard models.

116 e part in shaping topography, tectonics, and seismic hazard within intraplate settings.

117 stand earthquake interaction and to forecast seismic hazard.

118 l to understanding and appraising intraplate seismic hazard.

119 ments, potentially increasing the associated seismic hazard.

120 d physical models provide new ways to assess seismic hazards and forecast seismicity response to pert

121 s of the lower-mantle would exhibit enhanced seismic heterogeneities due to the occurrence of the mix

122 of the lower-mantle including the origin of seismic heterogeneities in the middle to lowermost parts

123 a unrest are still poorly reconstructed from seismic images.

124 Radar and seismic imaging combined with in situ borehole measureme

125 Seismic imaging reveals that these plumes can be of deep

126 Here we describe the use of a whole-mantle seismic imaging technique--combining accurate wavefield

127 field modelling is a key component of modern seismic imaging techniques, such as reverse-time migrati

128 w, we document our belief that Rothman had a seismic impact on moving investigative dermatology from

129 These seismic inferences are remarkably consistent with an ind

130 oint local and teleseismic earthquake P-wave seismic inversion, we revealed a basaltic lower-crustal

131 ), incipient melts probably trigger both the seismic low velocities and the high electrical conductiv

132 The seismic low velocities and the high electrical conductiv

133 locity to mean that hot plumes-which exhibit seismic low-velocity anomalies at depths of 200 kilometr

134 pot buoyancy fluxes and overlie regions with seismic low-velocity anomalies in the upper mantle, unli

135 Here, we propose a seismic metabarrier able to convert seismic Rayleigh wav

136 nsities and velocities in accord with radial seismic models, and leaves behind a silicate mantle that

137 rgest strike-slip earthquakes ever recorded (seismic moment magnitude M(w) 8.7) occurred about 100-20

138 Ambient-noise-based seismic monitoring of the near surface often has limited

139 Here we use passive seismic monitoring to examine mechanisms of iceberg disi

140 dy demonstrates the efficacy of near-surface seismic monitoring using DAS-recorded ambient noise.

141 Beginning on 24 April 2015, the seismic network captured an eruption that culminated in

142 from the Italian Strong Motion and National Seismic networks, and field measurements of surface rupt

143 In addition, our seismic noise analysis reveals an asymmetry and a high c

144 tissue characterization that is inspired by seismic noise correlation and time reversal.

145 fish exposed to playbacks of pile-driving or seismic noise for 12 weeks no longer responded with an e

146 e hysteresis in the high-frequency (5-15 Hz) seismic noise level relative to the associated hydrologi

147 and seismometers is challenged by background seismic noise, its robust detection with gravity gradiom

148 o longer responded to short-term playback of seismic noise.

149 thod for detecting changes in gas flux using seismic observations and provides a new tool for monitor

150 Seismic observations are interpreted using a geodynamic

151 Seismic observations in volcanically active calderas are

152 Here we use seismic observations to show that the most recent erupti

153 istence has been used to explain a number of seismic observations, such as the D'' reflector and the

154 loser to static failure, consistent with the seismic observations.

155 ost-perovskite assemblage is consistent with seismic observations.

156 s are ubiquitous at interfaces with optical, seismic or acoustic waves, and also with electron, neutr

157 Global seismic P wave recordings indicate a radiated seismic en

158 oratory experiments, numerical modeling, and seismic P-to-S conversions recorded by a dense seismic a

159 s, we find a relatively strong late-arriving seismic phase (dubbed Dam-forming phase or D-phase) reco

160 ault can slip in a single earthquake and the seismic potential of a partially coupled megathrust inte

161 ween our mineral physics predictions and the seismic Preliminary Reference Earth Model down to at lea

162 Mountains and available data from both deep seismic profiles and surface structural deformation.

163 ence of the normal faults interpreted in 3-D seismic profiles collected from adjacent areas.

164 wellhead pressure data, marine multichannel seismic profiles, seafloor and water-column sonar survey

165 together with bathymetry and high-resolution seismic profiles, were used to identify suitable samplin

166 boundary beneath southwest Okhotsk Sea with seismic properties intermediate between those of the inn

167 However, the observed seismic properties of lower crust and upper mantle in oc

168 Lateral variations in seismic properties on the slab surface suggest that serp

169 Scallop larvae exposed to playbacks of seismic pulses showed significant developmental delays a

170 y the Polochic fault during a long period of seismic quiescence, from 1450 to 1976 CE.

171 hich indicate that energetic, high-frequency seismic radiation originates from locations that are dis

172 oportionately large amount of high-frequency seismic radiation to be produced during fault rupture.

173 i earthquake was deficient in high-frequency seismic radiation--a difference that we attribute to its

174 loped to accurately describe and predict the seismic rainbow effect; allowing the metawedge to be des

175 es or reflect the Rayleigh waves creating a "seismic rainbow" effect analogous to the optical rainbow

176 of rocks at slip velocities approaching the seismic range ( approximately 0.1-1 m s(-1)), and at mod

177 e is highly-anisotropic and depending on the seismic ray path, its properties can be very difficult t

178 ropose a seismic metabarrier able to convert seismic Rayleigh waves into shear bulk waves that propag

179 al scale, the resonant metawedge, to control seismic Rayleigh waves.

180 We use EarthScope seismic receiver functions, gravity and surface heat flo

181 Continuous seismic records near river channels can be used to quant

182 Based on spectral characteristics of the seismic records, we also detected 20 landslide/debris fl

183 ts (DFLEs) in near real-time using broadband seismic records, which can provide timely warnings of th

184 ied iceberg scours seen in three-dimensional seismic reflection images from the mid-Norwegian slope.

185 When combined with a third seismic reflection profile of the western Himalayas, the

186 eometry provided by two newly obtained, deep seismic reflection profiles.

187 Our seismic results provide the first direct evidence that e

188 These seismic results suggest that, in the current thermo-comp

189 magma reservoir determined from multichannel seismic results.

190 Similar hysteresis has been observed between seismic river noise and discharge during storms, suggest

191 effectively defining the area of subsequent seismic rupture (rupture did not occur where slow slip w

192 eakening and promotes the propagation of the seismic rupture in carbonate-bearing fault patches.

193 tance for eruption forecasting the causes of seismic rupture processes during caldera unrest are stil

194 the earthquake, both up-dip and down-dip of seismic rupture.

195 ities, resulting in catastrophic failure and seismic rupture.

196 road range of engineering applications, from seismic shielding at low frequency to ultrasonic cloakin

197 Within recent years, there has been a seismic shift in smoking rates from high-income to low-

198 'non-volcanic' tremor, a recently discovered seismic signal probably generated by shear slip on the d

199 ges in microseismic monitoring is that those seismic signals generated from micro seismicity have ext

200 Exposure to seismic signals was found to significantly increase mort

201 ed together with high-frequency (HF, 1-3 Hz) seismic signals, we find a relatively strong late-arrivi

202 ortant bivalves, are affected by exposure to seismic signals.

203 re-insulating D" layer, but the absence of a seismic signature suggests the transition does not contr

204 itically needed to evaluate the composition, seismic signatures, and geodynamics of the planet's remo

205 Both aseismic and seismic slip accommodate relative motion across partiall

206 , the reason why, in continental domains, co-seismic slip along faults can propagate up to the Earth'

207 show that phyllosilicates can facilitate co-seismic slip along faults during earthquakes.

208 We confirm that some of the co-seismic slip at shallow depth (<5 km) constrained by InS

209 and experienced relatively minor (if any) co-seismic slip in 2011.

210 emonstrate that the observed variation of co-seismic slip is neither random nor artificial, but self-

211 We analyze high-resolution along-strike co-seismic slip profiles of the 1992 Mw = 7.3 Landers and 1

212 along micrometer-thick layers can facilitate seismic slip propagation during earthquakes in continent

213 Seismic slip propagation is facilitated by along-fault l

214 on zones, where pelagic clays participate in seismic slip propagation.

215 cular, rotary shear experiments conducted at seismic slip rates (1 ms(-1)) show that phyllosilicates

216 riction experiments, we demonstrate that, at seismic slip rates (1 ms(-1)), similar calcite gouges wi

217 Here, we demonstrate that at fast, seismic slip rates, an extraordinary reduction in the fr

218 eneous stress state that in turn controls co-seismic slip.

219 e we present high-resolution bathymetric and seismic sonar data sets of 10 morphologically similar dr

220 he geometry and the slip distribution of the seismic source and to compute the Coulomb Failure Functi

221 Seismic source locations and waveform attenuation analys

222 hese results suggest that interpretations of seismic structure in the deep mantle need to treat a bro

223 inental crust by calculating the density and seismic structure of two exposed sections of island arc

224 We interpret these seismic structures as a continuing regional, delaminatio

225 may reflect the degree-two lower mantle slow seismic structures.

226 Seismic studies identify a prominent velocity discontinu

227 incorporating constraints from a collocated seismic study into the magnetotelluric inversion process

228 Seismic surveys map the seabed using intense, low-freque

229 ts, we investigate the impact of exposure to seismic surveys on scallops, using measurements of physi

230 (playbacks of recordings of pile-driving and seismic surveys), but not to a more continuous additiona

231 g this hazard required analyses of 2D and 3D seismic surveys, seafloor bathymetry, sediment propertie

232 aseismic for two months just after the main seismic swarm (April 1, 1984) due to a SE-to-NW directed

233 Seismic swarms correlate in space and time with fluid in

234 eometry that can be monitored remotely using seismic techniques.

235 The seismic temporal increase is strongly correlated with th

236 ere-asthenosphere boundary, as inferred from seismic tomography and other geophysical studies.

237 Here we combine new seismic tomography and receiver function images to resol

238 Upper mantle features revealed by seismic tomography and that are apparently related to su

239 se is coincident in depth with regions where seismic tomography has imaged slab stagnation, plume def

240 microplates close to the trench, but recent seismic tomography studies have revealed a high-velocity

241 l lithosphere 175 kilometers thick, whereas seismic tomography supports a much thicker root (>250 ki

242 e, and be difficult to detect using standard seismic tomography techniques.

243 we use joint active-source/local-earthquake seismic tomography to derive unprecedented constraints o

244 oscience community is increasingly utilizing seismic tomography to interpret mantle heterogeneity and

245 Using full-waveform seismic tomography, we imaged a pattern of horizontally

246 nd the North Atlantic Ocean based on adjoint seismic tomography.

247 ep mantle remnants of subduction imaged with seismic tomography.

248 sociated with increases in SO2 emissions and seismic tremor.

249 rupture geometry, demonstrated likelihood of seismic triggering, and high model temperatures in young

250 oral characteristics and behavior similar to seismic tsunamis, is poorly understood.

251 Specifically, comparison between seismic V(P)--rho profiles of the core and candidate Fe

252 nated by linear abyssal hills, upper crustal seismic velocities abruptly increase by over 20%, and gr

253 Seismic velocities are commonly used to identify antigor

254 Low seismic velocities beneath the Central Lau Spreading Cen

255 a thermal calibration scale for interpreting seismic velocities located distant from ridges.

256 l distribution of partial melt inferred from seismic velocities obtained from Rayleigh wave tomograph

257 nosphere is associated with a platewide high-seismic velocity "lid" overlying lowered velocities, con

258 drock fracture distributions, as revealed by seismic velocity and electrical resistivity surveys from

259 We also reinterpret the high seismic velocity anomaly beneath the southern central va

260 antle asthenosphere corresponds to an abrupt seismic velocity decrease and electrical conductivity in

261 composition layer suggested by an anomaly in seismic velocity in the 150 kilometres immediately above

262 ble prediction of a post-seismic decrease of seismic velocity in the shallow crust of the affected re

263 present a continuous high-resolution crustal seismic velocity model for an 800 km section of the act

264 Our seismic velocity model indicates that the globally obser

265 flow measurements to estimate thickness and seismic velocity ratio, v(P)/v(S), of continental crust

266 and is characterized by a steady increase in seismic velocity similar to that observed in active arcs

267 topography-dependent tomographic scheme, the seismic velocity structure of the Eastern Tibetan Platea

268 s of the Earth is largely based on images of seismic velocity variations in the mantle obtained with

269 Detections of abrupt decreases in seismic velocity where downwelling mantle is inferred ar

270 Here we use seismic velocity, gravity and topography to generate a 3

271 zones and have an unusually low density and seismic velocity.

272 to the south, which has no distinct deep low-seismic-velocity anomalies.

273 This low-seismic-velocity anomaly becomes weaker with distance so

274 r function images to resolve a vertical high-seismic-velocity anomaly beneath the west-central platea

275 This suggests that a coincident seismic-velocity anomaly is evidence of shallow magma tr

276 Here we use seismic wave analyses to reveal that the 11 April 2012 e

277 Simulations of seismic wave propagation in sedimentary basins capture t

278 ificant seismic anisotropy, the variation of seismic wave speed with direction.

279 We use our data to model seismic wave velocities in the top portion of the lower

280 Seismic wave velocities, ocean ridge depths, and the com

281 an approximately 15 degrees dipping, abrupt, seismic wave-speed transition (less than 1 kilometre thi

282 Recent studies of seismic-wave receiver function data have detected a stru

283 at the bottom of the mantle, leading to low seismic-wave velocities and high electrical conductivity

284 Efficient numerical seismic wavefield modelling is a key component of modern

285 In seismic waveform tomography, or full-waveform inversion

286 Seismic waveforms for hypothetical underground nuclear e

287 utations with information contained in whole seismic waveforms--that reveals the presence of broad (n

288 Here we use explosion-generated seismic waves (of about 0.5-kilometre wavelength) to for

289 l earthquakes globally during passage of the seismic waves and during the following several hours to

290 Seismic waves can be generated by landquake events which

291 Sources of high-frequency seismic waves delineate the edges of the deepest portion

292 natural transient stresses generated by the seismic waves of large remote earthquakes.

293 The design allows controlling seismic waves with wavelengths from 10-to-100 m with met

294 rthquake rupture, even before the arrival of seismic waves.

295 systems imposed by the propagation speed of seismic waves.

296 ts of earthquakes by trapping and amplifying seismic waves.

297 rbonated silicate melt may contribute to the seismic X-discontinuity.

298 icroearthquakes in the intraplate New Madrid Seismic Zone at annual and multi-annual timescales coinc

299 Triggering in induced seismic zones could therefore be an indicator that fluid

300 It occurred near the edge of active seismic zones, similar to other M5+ earthquakes since 20