ライフサイエンスコーパス: earthquake

1 disaster scenario following a magnitude 8.0 earthquake.

2 was overcome, thereby generating the Lushan earthquake.

3 llow slip during the M(w)9.1 2011 Tohoku-Oki earthquake.

4 gy to accumulate to prepare for the next big earthquake.

5 fy the geodetic anomaly preceding the Lushan earthquake.

6 g the disaster response that follows a major earthquake.

7 even years before the 2011 Mw 9.0 Tohoku-Oki earthquake.

8 few years after the 2011 M(w) 9.0 Tohoku-Oki earthquake.

9 nt aquifers after the 2016 M(w) 7.0 Kumamoto earthquake.

10 ce of the 2011, moment magnitude 9.1, Tohoku earthquake.

11 han increased following the Great East Japan Earthquake.

12 e within one to two decades after each large earthquake.

13 atients presenting to TIO following repeated earthquake.

14 rection from the port of Kobe after the 1995 earthquake.

15 2.1%) conducted in 2013, 2.5 years after the earthquake.

16 ndslide under the excitation of the Wenchuan earthquake.

17 gered right-lateral slip during the M(w) 7.1 earthquake.

18 ) five years after the 2011 Great East Japan Earthquake.

19 due to interseismic loading and 25 > Mw 5.5 earthquakes.

20 gh strike-parallel channels while triggering earthquakes.

21 yles from stable sliding and creep events to earthquakes.

22 omplex interacting systems in nature such as earthquakes.

23 significant role in inhibiting or triggering earthquakes.

24 t topographic features and can produce large earthquakes.

25 easing energy equivalent to M (w) 4.7 to 5.4 earthquakes.

26 blocks can control the slip velocity during earthquakes.

27 re comparable to observed values of moderate earthquakes.

28 terials and the preparation process of large earthquakes.

29 tanding of deep Earth dynamics and submarine earthquakes.

30 mescales of post-seismic healing observed in earthquakes.

31 akening mechanism during natural and induced earthquakes.

32 sound waves that are generated by repeating earthquakes.

33 attempting to identify the sources of major earthquakes.

34 predicting the rupture zone of future large earthquakes.

35 nough stress is transferred upwards by blind earthquakes.

36 causes fluid pressure transients that induce earthquakes.

37 an rupture propagation for small to moderate earthquakes.

38 power law scaling in magnitude, as found in earthquakes.

39 sm is consistent with observations of hybrid earthquakes.

40 ting stress changes on fault planes of small earthquakes.

41 describe water provenances before and after earthquakes.

42 submitted by tens of millions of users after earthquakes.

43 ties can change in response to large crustal earthquakes.

44 primary contributor to tsunami generation by earthquakes.

45 eation that remain elusive for classic, fast earthquakes.

46 pagating rupture fronts that are essentially earthquakes.

47 and intensity distributions for most of the earthquakes.

48 Intermediate-depth earthquakes (30-300 km) have been extensively documented

49 llowing the duration-cubed scaling found for earthquakes(9).

50 e data, we infer that during large magnitude earthquakes a step-over along the fault zone results in

51 fort resulted in a catalog with 1.81 million earthquakes, a 10-fold increase, which provides importan

52 ially tsunamigenic landslides likely through earthquake activity and enhanced sediment supply.

53 cal surface gravity waves, and a teleseismic earthquake along a 4192-sensor ocean-bottom DAS array of

54 e part of a long-lived cluster of historical earthquakes along the Eastern California Shear Zone (ECS

55 d Turkey that focused on improving household earthquake and fire preparedness.

56 afloor slope sediments triggered by the 2011 earthquake and its aftershock sequence.

57 even months before the 2011 Great East Japan Earthquake and Tsunami in a survey of older community-dw

58 Improving earthquake and tsunami risk assessment requires understa

59 pite the 1-hour warning interval between the earthquake and tsunami, many coastal residents lost thei

60 older survivors of the 2011 Great East Japan earthquake and tsunami.

61 elocation in the aftermath of the 2011 Japan Earthquake and Tsunami.

62 tly in the line of the 2011 Great East Japan Earthquake and Tsunami.

63 lowing exposure to the 2011 Great East Japan Earthquake and Tsunami.

64 ts who experienced the 2011 Great East Japan Earthquake and Tsunami.

65 ortable (3)He/(4)He ratio detectors aimed at earthquake and volcanic eruption studies, and monitoring

66 0 seismograms (250k associated with tectonic earthquakes and 250k identified as noise) recorded in No

67 ed for detection of regional and teleseismic earthquakes and evaluated for long period response using

68 acilitate the next generation of analyses of earthquakes and faults.

69 pre-stress (the cumulative CST from multiple earthquakes and interseismic loading on non-planar fault

70 he current locations of the highest rates of earthquakes and prominent low shear velocities, whereas

71 improve traffic-light protocols for induced earthquakes and the regulation of operational injection

72 Historical and sediment records of large earthquakes and tsunamis have expanded the temporal data

73 and now geologic evidence suggest that great earthquakes and tsunamis have whipped the Pacific coast

74 underestimated as potential source for great earthquakes and tsunamis.

75 nking collapses) and physical systems (e.g., earthquakes), and yet it remains unclear the extent to w

76 ic displacements caused by the 2008 Wenchuan earthquake, and after transforming the reference frame a

77 The 1787 earthquake, and tsunami and a probable predecessor in 15

78 al motions and that of other normal faulting earthquakes, and (b) for the first time model the levell

79 r the stress-loading of faults to failure in earthquakes appears to be random or to an extent explain

80 These earthquakes are depleted in high-frequency content and t

81 Waves from deep earthquakes are easier to pick, but the S/N ratio can be

82 Therefore, to understand better when large earthquakes are imminent, we must consider not only the

83 p compression is observed, we argue that the earthquakes are mapping the top and bottom of the slab.

84 s, 40% of the global population at risk from earthquakes are obscured from optical satellite view for

85 Deep intracontinental earthquakes are poorly understood, despite their potenti

86 Megathrust earthquakes are responsible for some of the most devasta

87 ayas, such as that following the 2015 Gorkha earthquake, are unlikely to drive increased gravel aggra

88 orizontal strain rate zone can have as large earthquakes as high horizontal strain rate zones, just w

89 We infer that the occurrence of the giant earthquake at the shallow portion of the megathrust may

90 Our understanding of the frequency of large earthquakes at timescales longer than instrumental and h

91 Faults can slip not only episodically during earthquakes but also during transient aseismic slip even

92 Here we decipher the mechanism of these earthquakes by performing deformation experiments on deh

93 lip frictional instability-the mechanism for earthquakes-by carrying out a linear stability analysis

94 on of healthcare demands mismatches the post-earthquake capacities of hospitals, leaving large zones

95 In establishing rate changes, short duration earthquake catalogs are commonly used, and triggered seq

96 Earthquake catalogs are thus dominated by small earthqua

97 mainshocks and four western USA 33-yearlong earthquake catalogs, we compare the ability of three dif

98 The ability to predict the magnitude of an earthquake caused by deep fluid injections is an importa

99 Moderate to large induced earthquakes, causing widespread hazards, are often relat

100 uring the 30(th) October 2016 Mw 6.6 Vettore earthquake (Central Italy), using low-cost Global Naviga

101 At about 40 days before, two earthquakes clusters started, with one M3 earthquake occ

102 ismite unit, also produced by a major palaeo-earthquake, comprises clastic dikes that cut through the

103 ulations reproduce important features of the earthquake cycle, including interseismic strain and a bi

104 ain markers accumulating the effects of many earthquake cycles help to constrain the mechanical behav

105 the build-up and release of stress over many earthquake cycles, is a key question for seismic hazard

106 tifies multiseverity injuries as a result of earthquake damage.

107 This complex earthquake defies many conventional assumptions about th

108 e laboratory analogues of intermediate-depth earthquakes demonstrate that little dehydration is requi

109 We find that the likelihood of triggering earthquakes depends largely on the rate of increase in p

110 ty at Axial Volcano results from the shallow earthquake depths.

111 global deep-learning model for simultaneous earthquake detection and phase picking.

112 Here, we introduce the Cnn-Rnn Earthquake Detector (CRED), a detector based on deep neu

113 ing for cloud, the worst time of year for an earthquake disaster is between June and August.

114 Deep long-period earthquakes (DLPs) are an enigmatic type of volcanic sei

115 However, earthquakes do tend to occur where the cumulative coseis

116 istribution of the observed magnitude (M) 3+ earthquakes during 2008-2017 is reproducible and is the

117 We explore how accurate earthquake early warning (EEW) can be, given our limited

118 es fault permeability, and is released after earthquakes enhance permeability.

119 arthquake science by triggering the study of earthquake environmental effects worldwide, yet its sour

120 Earthquakes far from tectonic plate boundaries generally

121 ime search engine queries to efficiently map earthquake felt area in the regions with a relatively la

122 es of hazard monitoring (such as landslides, earthquakes, floods), especially those with meager occur

123 g the effect of natural hazard events (e.g., earthquakes, floods, hurricanes) on assets, people and s

124 Earthquakes follow a well-known power-law size relation,

125 On July 4 2019, a M(w) 6.5 earthquake, followed 34 h later by a M(w) 7.1 event, str

126 ude of earthquakes is required for effective earthquake forecasting.

127 ed in a range of complex phenomena including earthquakes, forest fires and solar flares.

128 xercises control on the production of magma, earthquakes, formation of continental crust and mineral

129 ce intervals and to test competing models of earthquake frequency (e.g., time-dependent, time-indepen

130 nhanced through filtering and the data cover earthquakes from all depths.

131 smic waves from the magnitude M(w) ~10 to 11 earthquake generated by the Chicxulub impact, identifyin

132 veral scenarios involving large tsunamigenic earthquakes generated by ruptures along segments of the

133 better understand the physical mechanisms of earthquake generation, subduction zones worldwide are co

134 The giant 2011 Tohoku-oki earthquake has been inferred to remobilise fine-grained,

135 e strong tidal triggering of mid-ocean ridge earthquakes has remained unexplained because the earthqu

136 records and indicate that large tsunamigenic earthquakes have shaken the Guerrero-Oaxaca region in so

137 Contemporary earthquake hazard models hinge on an understanding of ho

138 On May 1, 2018, a magnitude 5.0 earthquake heralded the collapse of the Pu'u O'o Vent on

139 10 m, and each could have hosted many great earthquakes, illustrating an extensive history of great

140 he types of ocular injuries sustained in the earthquake in Nepal and its management in Tilganga Insti

141 the 2018-08-19 [Formula: see text] Fiji deep earthquake in the 0.01-1 Hz frequency band, though wavef

142 n all-cause heat-related mortality after the earthquake in the 15 prefectures with the greatest reduc

143 Major earthquakes in California have occurred above the region

144 by study of a 667-year historical record of earthquakes in central Italy.

145 monstrates that the distribution and size of earthquakes in Italy correlates with the steady state ra

146 continuous data recorded during 2000 Tottori earthquakes in Japan, we were able to detect and locate

147 n of ocular trauma resulting from the recent earthquakes in Nepal has not been described thus far.

148 ffects, is the primary driver of the induced earthquakes in Oklahoma.

149 demonstrate the importance of the timing of earthquakes in terms of our capacity to respond effectiv

150 s accumulation and release, leading to large earthquakes in the Longmenshan area.

151 ed to potential sources of future megathrust earthquakes in the region.

152 ma the relative proportion of high-magnitude earthquakes increases at 8+ km depth.

153 These findings indicate that earthquake-induced sediment pulses sourced from the Grea

154 roach to develop a rupture scenario for this earthquake, informed by the damage distribution.

155 duced seismicity: pore pressure increase and earthquake interactions lead to fault weakening and ulti

156 static stress transfer modeling reveals that earthquake interactions promote continued seismicity, le

157 Our results suggest that the Pawnee earthquake is a result of interplay among injection, tec

158 lution of slip on surface ruptures during an earthquake is important for assessing fault displacement

159 nge of normal stress on the fault before the earthquake is not uniform but increases in the up-dip po

160 The Pawnee M5.8 earthquake is the largest event in Oklahoma instrument r

161 The triggering and magnitude of earthquakes is determined by the friction evolution alon

162 the best-preserved topographic signature of earthquakes is expected to occur early in the postseismi

163 Stress-loading to failure in earthquakes is not the same for all faults and is depend

164 ontrols on the distribution and magnitude of earthquakes is required for effective earthquake forecas

165 on transient following large subduction zone earthquakes is thought to originate from the interaction

166 t weakening and ultimately triggering larger earthquakes later in the process.

167 rican Great Plains exemplify such intraplate earthquake localization, with both natural and induced s

168 limitations, EEW can significantly mitigate earthquake losses for false-alert-tolerant users who cho

169 etwork in Oaxaca, we identified 20 swarms of earthquakes (M < 5) from 2006 to 2012.

170 Successive locations of individual large earthquakes (M(w) > 5.5) over years to centuries can be

171 mi deposit is associated with the 1787 great earthquake, M 8.6, producing a giant tsunami that poured

172 A recent major earthquake (M7.8), coupled with appropriate climatic con

173 be the most common EEW outcome even when the earthquake magnitude and location are accurately determi

174 for a highly valuable rapid estimate of the earthquake magnitude.

175 and destructive potential of impact-induced earthquakes may be underestimated.

176 reductions, the frequency of high-magnitude earthquakes may decay more slowly than the overall earth

177 Pre-earthquake mean maximum monthly temperature and post-ear

178 ke mean maximum monthly temperature and post-earthquake mean monthly pressure were negatively associa

179 dipping at ~30 degrees down to ~600 km, and earthquake mechanisms point to down-dip compression.

180 tial injection rate reductions, the downward earthquake migration rate slowed to ~0.1 km per year.

181 While most earthquake models assume a fixed pore fluid pressure dis

182 y align with those observed independently in earthquake moment tensors and borehole breakouts.

183 A 4 May earthquake [moment magnitude (M (w)) 6.9] produced ~5 me

184 We leverage advances in earthquake monitoring with a deep-learning algorithm to

185 nt for our fundamental understanding of both earthquake motion and the most general types of friction

186 ed in and around the epicenter of the Lushan earthquake (Mw 6.7), which occurred almost 5 years after

187 The 28th December 1908 Messina earthquake (Mw 7.1), Italy, caused >80,000 deaths and tr

188 The ~680 km deep 2015 Bonin earthquake (Mw~7.9) is located at the northernmost edge

189 e seismogenic zone, whereas infrequent great earthquakes (Mw 8+) propagate up to the Himalayan fronta

190 gh a case study of the 2017 M(w) 5.5 induced earthquake near Pohang Enhanced Geothermal System, Korea

191 4 July 2019 with a sequence of intersecting earthquakes near the city of Ridgecrest, California.

192 achylytes represent direct identification of earthquake nucleation as a transient consequence of ongo

193 end, here we develop a poroelastic model of earthquake nucleation based on rate-and-state friction i

194 lip-rate (V), fault geometry (L/H(0)(2)) and earthquake nucleation depth (~sigma(eff))), EHD might be

195 e seismic moment in the total compilation of earthquakes observed during these experiments.

196 liver fault suggests that SSEs and swarms of earthquakes occur due to high fluid content in the fault

197 Faulting and earthquakes occur extensively along the flanks of the Ea

198 The largest observed earthquakes occur on subduction interfaces and frequentl

199 hquakes has remained unexplained because the earthquakes occur preferentially during low tide, when n

200 It is generally believed that earthquakes occur when faults weaken with increasing sli

201 wo earthquakes clusters started, with one M3 earthquake occurred two days before the mainshock.

202 By fitting the epicenters of earthquakes occurred in mainland China from 2014 to 2018

203 We found that the probability of earthquakes occurring is linked to S by a linear correla

204 seismological analyses of the 2016 M(w) 6.4 earthquake offshore Morocco - the largest event ever rec

205 Large, destructive earthquakes often propagate along thrust faults includin

206 s, shedding new light on the impact of large earthquakes on long-term carbon cycling in the deep-sea.

207 on megathrust and bear strong resemblance to earthquakes, only slower.

208 ctivation of power-law creep during the post-earthquake period.

209 This model can be used to assess earthquake potential on specific fault segments.

210 ntervention groups, with more improvement in earthquake preparedness in the Turkish participants and

211 l injection shut-in in April 2017 causes the earthquake probability to approach its background level

212 records suggests that the Mexican Subduction earthquakes produce relatively small tsunamis, however h

213 We discovered two independent earthquake-produced seismite horizons in North Alpine Fo

214 e, although there are notable examples where earthquake propagate across negatively stressed portions

215 aterial and structural conditions that favor earthquake propagation to the trench.

216 During earthquake propagation, geologic faults lose their stren

217 rwhelm the former, explaining why historical earthquakes rarely rupture nearest neighbor faults.

218 from statistically significant increases in earthquake rate coincident with the passage of seismic e

219 uakes may decay more slowly than the overall earthquake rate.

220 Relocation of earthquakes recorded by the agency for meteorology, clim

221 urred almost 5 years after the 2008 Wenchuan earthquake, recorded preseismic deformation correspondin

222 Here we investigate earthquake recurrence for a system of 25 active normal f

223 s are required both to better quantify their earthquake recurrence intervals and to test competing mo

224 s been limited until now, because intraplate earthquake recurrence intervals are generally long (10s

225 Long-term variations in the earthquake recurrence intervals of intraplate faults the

226 n sandsheet emplacement or that tsunamigenic earthquake recurrence may have been more frequent in the

227 following the 1999 Chi-Chi and 2008 Wenchuan earthquakes reduced channel capacity and increased flood

228 ausal mechanisms for fluid injection-induced earthquakes remain a challenge to identify.

229 year and consequently contribute to overall earthquake risk.

230 ctional-mechanical processes associated with earthquake rupture cycles, but there are few temperature

231 Whether the earthquake rupture extended to the shallow part of the p

232 along the 2014 M 6.0 South Napa, California, earthquake rupture, each dominated by either co- or post

233 tional assumptions about the degree to which earthquake ruptures are controlled by fault segmentation

234 The asymmetric interaction of thrust earthquake ruptures with the free surface leads to sudde

235 Italy, caused >80,000 deaths and transformed earthquake science by triggering the study of earthquake

236 Here we use joint active-source/local-earthquake seismic tomography to derive unprecedented co

237 , illustrating an extensive history of great earthquake seismicity that caused large shallow slip.

238 ing of both near-surface soil properties and earthquake seismology.

239 r fractures) surrounding the 2019 Ridgecrest earthquake sequence.

240 ere we present a numerical modeling study of earthquake sequences and aseismic transient slip on ocea

241 g through 2-D antiplane shear simulations of earthquake sequences on a strike-slip fault with rate-an

242 g for climatic and socioeconomic conditions, earthquake severity was associated with incident ZIKV ca

243 tially during low tide, when normal faulting earthquakes should be inhibited.

244 Investigation of the slopes in the Wenchuan earthquake shows that tension failures appear in the upp

245 Earthquake signal detection and seismic phase picking ar

246 Earthquake signal detection is at the core of observatio

247 characteristics of the dominant phases in an earthquake signal from three component data recorded on

248 mation in phases and in the full waveform of earthquake signals by using a hierarchical attention mec

249 odel with respect to the noise level and non-earthquake signals is shown by applying it to a set of s

250 m shapes, robust to background noise and non-earthquake signals, and efficient for processing large d

251 Such strength could enable earthquake slip at high differential stress within a pre

252 Like regular earthquakes, slow-slip events also have a moment that is

253 ity to forecast expected shaking even if the earthquake source is known.

254 ed aseismic deformation, and the distance of earthquake sources from injection.

255 g failure and, more generally, complexity of earthquake sources.

256 We predict, with a model (earthquake stress model) that inverts the displacements

257 In April 2016, the Kumamoto earthquake struck the region.

258 thus strikingly similar to those of regular earthquakes, suggesting that they are governed by simila

259 reversal that occurred before the Tohoku-oki earthquake suggests an initial slow slip followed by a s

260 ationship of seismite formation during large earthquakes suggests the seismic and destructive potenti

261 nt Agung and Batur Caldera that initiated an earthquake swarm in late September.

262 , triggering shallow creep and a substantial earthquake swarm.

263 The vibrant evolutionary patterns made by earthquake swarms are incompatible with standard, effect

264 Earthquake swarms attributed to subsurface fluid injecti

265 ip near the base of the seismogenic zone and earthquake swarms within the seismogenic zone, as ascend

266 fy the relation between aseismic fault slip, earthquake swarms, and fault zone hydromechanical proper

267 the majority of the population at risk from earthquakes that could be obscured by cloud in every mon

268 in many false alerts (unnecessary alerts for earthquakes that do not produce damaging ground shaking)

269 between the S and the magnitude of M >= 2.5 earthquakes that occurred in the same period of satellit

270 11 March 1933 Mw 6.4 Long Beach, California, earthquake, the largest known earthquake within the cent

271 Immediately after a destructive earthquake, the real-time seismological community has a

272 ocess causal mechanism for injection-induced earthquakes through a case study of the 2017 M(w) 5.5 in

273 rupture model of the 2016 M(w) 7.8 Kaikoura earthquake to unravel the event's riddles in a physics-b

274 In northern Oklahoma, this effect caused earthquakes to migrate downward at ~0.5 km per year duri

275 The occurrence of the M(w) 6.4 earthquake together with historical and instrumental eve

276 for the first time the spatial extent of the earthquake-triggered event deposit along the hadal Japan

277 Remote earthquake triggering is a well-established phenomenon.

278 ar faults is an ignored yet vital factor for earthquake triggering.

279 erent statistical methods to identify remote earthquake triggering.

280 shock behavior and nucleation processes, and earthquake-triggering mechanisms.

281 ht outpace pore-fluid migration and transmit earthquake-triggering stress changes beyond the fluid-pr

282 h Pacific Tsunami and the 1960 Great Chilean Earthquake Tsunami.

283 e Himalayan seismicity can be bimodal: blind earthquakes (up to Mw ~ 7.8) tend to cluster in the down

284 field of the 24 August 2014 M6.0 South Napa earthquake using SAR data from the Italian Space Agency'

285 ere able to detect and locate two times more earthquakes using only a portion (less than 1/3) of seis

286 Recordings of a minor earthquake wavefield identified multiple submarine fault

287 constrain the geometry and kinematics of the earthquake we use elastic half-space modelling on non-pl

288 and PKP waves from regional and teleseismic earthquakes were observed for a range of magnitudes.

289 011 Tohoku-oki, Japan (moment magnitude 9.0) earthquakes were preceded by reversals of 4-8 millimetre

290 ions of shear and normal stresses before the earthquake, which match the ruptured areas of the mainsh

291 ificantly larger than the 2015 Mw 7.8 Gorkha earthquake, which should be accounted for in future seis

292 sity pattern supports the association of the earthquake with the Newport-Inglewood fault; it further

293 repeating magnitude (M) [Formula: see text] earthquakes with abundant foreshocks and seismic swarms,

294 esults show that multiple faults have hosted earthquakes with displacement >= 10 m, and each could ha

295 ynamic friction, which may be reduced during earthquakes with high slip rates, a process known as sli

296 function (STF) data sets for subduction zone earthquakes, with moment magnitude Mw >/= 7, and show th

297 ntifiable precursor to forecast an impending earthquake within a period of less than two and half yea

298 h, California, earthquake, the largest known earthquake within the central Los Angeles Basin region.

299 smic deformation corresponding to the Lushan earthquake within the southern Longmenshan thrust belt.

300 thquake catalogs are thus dominated by small earthquakes yet are still missing a much larger number o