ライフサイエンスコーパス: seismic wave

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

2 systems imposed by the propagation speed of seismic waves.

3 ity in the direction of fast propagation for seismic waves.

4 ts of earthquakes by trapping and amplifying seismic waves.

5 ing aftershocks being nearly proportional to seismic wave amplitude.

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

7 ust faulting only being revealed by detailed seismic wave analyses.

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

9 scale-free dynamics in nature, such as earth seismic waves and stock market fluctuations, suggesting

10 tress changes associated with the passage of seismic waves are thought to trigger earthquakes at grea

11 Long-period seismic waves are thus useful for detecting and studying

12 the observed range dependence in long-period seismic wave arrivals that reflect off of these interfac

13 A. Hart, a man jumping at 1.11 km propagated seismic waves at 10-40 Hz.

14 hat the damage resulted from the focusing of seismic waves by several underground acoustic lenses at

15 Seismic waves can be generated by landquake events which

16 ins unknown how the small strains induced by seismic waves can trigger earthquakes at large distances

17 cillatory 'dynamic' deformations radiated as seismic waves can trigger seismicity rate increases, as

18 m these we infer that, if the fault is weak, seismic waves cause the fault core modulus to decrease a

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

20 c anisotropy is present where the speed of a seismic wave depends on its direction.

21 The characteristics of seismic waves detected at the Large Aperture Seismic Arr

22 significantly lowered if the pressure of the seismic wave drives a volume-reducing phase transformati

23 The spreading properties of seismic waves favor long-distance propagation for commun

24 not correspond to arrival times of the main seismic waves from the mainshocks and the dynamically tr

25 rshocks that occur before the arrival of the seismic wave front from the mainshock, which violates ca

26 namically weakened faults may fail after the seismic waves have passed by, and might even cause earth

27 n provides an additional explanation for the seismic wave heterogeneity in the lowermost mantle.

28 does not make a significant contribution to seismic-wave heterogeneity of the lower mantle.

29 The velocities of seismic waves in the Earth are governed by the response

30 The attenuation of seismic waves in the inner core is strong, and studies o

31 near behaviour of fault gouge perturbed by a seismic wave may trigger earthquakes, even with such sma

32 speculate that fault damage caused by strong seismic waves may help to explain earthquake clustering

33 reas dynamic (transient) stresses carried by seismic waves may trigger earthquakes both nearby and at

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

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

36 Decreases in the velocity of seismic waves passing through the fault zone due to cose

37 Simulations of seismic wave propagation in sedimentary basins capture t

38 computed from a hybrid method, which handles seismic wave propagation through two-dimensional complex

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

40 Seismic wave reflections from Earth's core recorded at s

41 The recent detection of seismic waves scattered in the inner core suggests a sim

42 Here we present observations of seismic waves scattered in the inner core which follow t

43 s of an anomalous precursor to the reflected seismic wave ScP reveal compressional and shear-wave vel

44 Here we present array-based observations of seismic waves sensitive to this part of the core whose w

45 Dynamic triggering by seismic waves should be enhanced in directions where rup

46 tle, that are detected as discontinuities in seismic wave speed and for which the pressure and temper

47 lowermost mantle have been observed to have seismic wave speed reductions of at least 10 per cent, w

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

49 But trade-offs between seismic wave-speed heterogeneity and discontinuity topog

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

51 e Earth are strongly anisotropic in terms of seismic-wave speeds.

52 uld be large enough to inhibit triggering by seismic-wave stress perturbations.

53 e in the travel times and wave forms of P4KP seismic waves that reflect internally in the core.

54 Seismic waves that traverse Earth's inner core along nor

55 t, oscillatory stress changes transmitted as seismic waves (that is, 'dynamic' stresses).

56 The propagation of seismic waves through Earth can now be modeled accuratel

57 Ocean waves couple into seismic waves through the quadratic nonlinearity of the

58 Earthquakes generate two seismic wave types: compressional (P) and shear (S) wave

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

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

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

62 roach is to exploit the stress dependence of seismic wave velocity, and we have investigated this in

63 els, such as three-dimensional variations of seismic wave velocity, density, and crustal thickness.

64 --in particular, a directional dependence in seismic-wave velocity.

65 out 0.01 s per year in the separation of two seismic waves with differing paths through the core.

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

67 ns (the stresses and strains associated with seismic waves) with distance from, and magnitude of, the