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1 rthquake rupture, even before the arrival of seismic waves.
2  seismometers in Japan before the arrival of seismic waves.
3  systems imposed by the propagation speed of seismic waves.
4 ts of earthquakes by trapping and amplifying seismic waves.
5 ity in the direction of fast propagation for seismic waves.
6  propagate into the ground as high-frequency seismic waves.
7 at propagate along tectonic faults and cause seismic waves.
8 dary in certain regions using scattered P'P' seismic waves.
9  and latency associated with the slowness of seismic waves.
10 the fault zone and subordinately as radiated seismic waves.
11 ing aftershocks being nearly proportional to seismic wave amplitude.
12                                  Here we use seismic wave analyses to reveal that the 11 April 2012 e
13 ust faulting only being revealed by detailed seismic wave analyses.
14 l earthquakes globally during passage of the seismic waves and during the following several hours to
15 scale-free dynamics in nature, such as earth seismic waves and stock market fluctuations, suggesting
16 tress changes associated with the passage of seismic waves are thought to trigger earthquakes at grea
17                                  Long-period seismic waves are thus useful for detecting and studying
18 the observed range dependence in long-period seismic wave arrivals that reflect off of these interfac
19 A. Hart, a man jumping at 1.11 km propagated seismic waves at 10-40 Hz.
20 hat the damage resulted from the focusing of seismic waves by several underground acoustic lenses at
21                                              Seismic waves can be generated by landquake events which
22                                Scattering of seismic waves can reveal subsurface structures but usual
23 ins unknown how the small strains induced by seismic waves can trigger earthquakes at large distances
24 cillatory 'dynamic' deformations radiated as seismic waves can trigger seismicity rate increases, as
25 m these we infer that, if the fault is weak, seismic waves cause the fault core modulus to decrease a
26                    Sources of high-frequency seismic waves delineate the edges of the deepest portion
27 c anisotropy is present where the speed of a seismic wave depends on its direction.
28                       The characteristics of seismic waves detected at the Large Aperture Seismic Arr
29 significantly lowered if the pressure of the seismic wave drives a volume-reducing phase transformati
30      Standard early warning systems based on seismic waves fail to rapidly estimate the size of such
31 ith the wrong mainshock time and those using seismic waves far from the Norcia mainshock; both show d
32                  The spreading properties of seismic waves favor long-distance propagation for commun
33 ority is generated by the interaction of the seismic wave field with three-dimensional heterogeneity
34 strike-slip faulting mechanism inferred from seismic waves for the aftershock, it generated much larg
35                                              Seismic waves from earthquakes and other sources are use
36                                              Seismic waves from earthquakes can be used to image the
37                   We detected reflections of seismic waves from the core-mantle boundary of Mars usin
38 nstead consistent with the arrival of strong seismic waves from the magnitude M(w) ~10 to 11 earthqua
39  not correspond to arrival times of the main seismic waves from the mainshocks and the dynamically tr
40 rshocks that occur before the arrival of the seismic wave front from the mainshock, which violates ca
41 namically weakened faults may fail after the seismic waves have passed by, and might even cause earth
42 n provides an additional explanation for the seismic wave heterogeneity in the lowermost mantle.
43  does not make a significant contribution to seismic-wave heterogeneity of the lower mantle.
44                            The velocities of seismic waves in the Earth are governed by the response
45                           The attenuation of seismic waves in the inner core is strong, and studies o
46 ations at the seafloor capable of generating seismic waves in the solid Earth.
47 asurements of travel times and amplitudes of seismic waves interacting with mineralogical phase trans
48 ggering of slow slip events (SSE) by passing seismic waves involve seismological questions with impor
49 near behaviour of fault gouge perturbed by a seismic wave may trigger earthquakes, even with such sma
50 speculate that fault damage caused by strong seismic waves may help to explain earthquake clustering
51 reas dynamic (transient) stresses carried by seismic waves may trigger earthquakes both nearby and at
52 ural heterogeneities which strongly scatters seismic waves obscuring the ballistic arrivals normally
53 n the Earth of ~2.0 x 10(13) N that radiated seismic waves observed throughout the planet, with ~25 s
54  natural transient stresses generated by the seismic waves of large remote earthquakes.
55 ubject to the "traumatic" stress produced by seismic waves of the great 2017 (Mw8.2) Tehuantepec eart
56              Here we use explosion-generated seismic waves (of about 0.5-kilometre wavelength) to for
57  for an ergodic model that explains observed seismic wave partitioning, a requirement for full-wave f
58                 Decreases in the velocity of seismic waves passing through the fault zone due to cose
59 show that DL models successfully distinguish seismic waves pre/post mainshock in accord with lab and
60 seismogram of this event, we have identified seismic wave precursors, i.e., underside reflections off
61         We present the first observations of seismic waves propagating through the core of Mars.
62  Using numerical simulations of global-scale seismic wave propagation at unprecedented high frequency
63 dium to propagate ultrasonic waves, to mimic seismic wave propagation from local earthquakes.
64                               Simulations of seismic wave propagation in sedimentary basins capture t
65                                     Studying seismic wave propagation through complex media is crucia
66 computed from a hybrid method, which handles seismic wave propagation through two-dimensional complex
67                                      Distant seismic waves provide clues to the evolution of crustal
68                            Recent studies of seismic-wave receiver function data have detected a stru
69   This study examines the characteristics of seismic wave reflection and wave-induced fluid flow (WIF
70                                              Seismic wave reflections from Earth's core recorded at s
71 lf of the diffracting waveforms, we detected seismic waves scattered by three-dimensional structures
72                      The recent detection of seismic waves scattered in the inner core suggests a sim
73              Here we present observations of seismic waves scattered in the inner core which follow t
74 s of an anomalous precursor to the reflected seismic wave ScP reveal compressional and shear-wave vel
75  Here we present array-based observations of seismic waves sensitive to this part of the core whose w
76                        Dynamic triggering by seismic waves should be enhanced in directions where rup
77 tle, that are detected as discontinuities in seismic wave speed and for which the pressure and temper
78 w velocity provinces" (LLVPs) are broad, low seismic wave speed anomalies in Earth's lower mantle ben
79  lowermost mantle have been observed to have seismic wave speed reductions of at least 10 per cent, w
80 ificant seismic anisotropy, the variation of seismic wave speed with direction.
81                       But trade-offs between seismic wave-speed heterogeneity and discontinuity topog
82 an approximately 15 degrees dipping, abrupt, seismic wave-speed transition (less than 1 kilometre thi
83                                  The slowest seismic wave speeds (shear wave speed less than 2.3 kilo
84 e Earth are strongly anisotropic in terms of seismic-wave speeds.
85                Full-waveform tomography maps seismic wave-speeds inside the Earth in three dimensions
86 uld be large enough to inhibit triggering by seismic-wave stress perturbations.
87                                       We use seismic waves that pass through the hypocentral region o
88 e in the travel times and wave forms of P4KP seismic waves that reflect internally in the core.
89                                              Seismic waves that traverse Earth's inner core along nor
90 t, oscillatory stress changes transmitted as seismic waves (that is, 'dynamic' stresses).
91                           The propagation of seismic waves through Earth can now be modeled accuratel
92                      Ocean waves couple into seismic waves through the quadratic nonlinearity of the
93 eveal the conversion of primary to secondary seismic waves to image the discontinuities that bound th
94                     Earthquakes generate two seismic wave types: compressional (P) and shear (S) wave
95                     We use our data to model seismic wave velocities in the top portion of the lower
96 urface stress state by monitoring changes in seismic wave velocities over an 11-year period.
97 zation leads to changes in the bulk modulus, seismic wave velocities, and proton mobility and plays a
98                                              Seismic wave velocities, ocean ridge depths, and the com
99  at the bottom of the mantle, leading to low seismic-wave velocities and high electrical conductivity
100 roach is to exploit the stress dependence of seismic wave velocity, and we have investigated this in
101 els, such as three-dimensional variations of seismic wave velocity, density, and crustal thickness.
102 --in particular, a directional dependence in seismic-wave velocity.
103 out 0.01 s per year in the separation of two seismic waves with differing paths through the core.
104                The design allows controlling seismic waves with wavelengths from 10-to-100 m with met
105 ns (the stresses and strains associated with seismic waves) with distance from, and magnitude of, the

 
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