ライフサイエンスコーパス: low-velocity

1 rate and state theory of dynamic friction at low velocities.

2 Relatively low velocity (10 to 30%), high electrical conductivity,

3 a exchange, is dominated by wave breaking at low velocities and short wavelengths.

4 ient melts probably trigger both the seismic low velocities and the high electrical conductivities in

5 The seismic low velocities and the high electrical conductivities of

6 velocity and provides an explanation to the low-velocity and ultra-low-velocity zones.

7 o mean that hot plumes-which exhibit seismic low-velocity anomalies at depths of 200 kilometres-are m

8 ancy fluxes and overlie regions with seismic low-velocity anomalies in the upper mantle, unlike plume

9 In contrast, a low velocity anomaly beneath Iceland is confined to the

10 ty variations in the mantle reveals a tilted low velocity anomaly extending from the core-mantle boun

11 and land seismometers, show an upper-mantle low-velocity anomaly that is elongated in the direction

12 st as approximately 400 mus are measured for low velocity ( approximately 0.1 m/s) collisions of drop

13 (approximately 47) short-duration (<15 min), low-velocity ( approximately 1 mph) walking bouts.

14 We detect localized low velocities at the edge of the slab material, which m

15 t rats were injured by either weight drop or low-velocity ballistic trauma and assessed by clinical e

16 Low-velocity ballistic trauma to the inferior sclera cre

17 s a several-hundred-kilometer-wide region of low velocities beneath and southeast of Hawaii.

18 such systems are known to produce relatively low-velocity bipolar outflows.

19 nge' lamina I spinoparabrachial neurons were low velocity brush strokes: peak discharge occurred at a

20 We conclude that gentle, low-velocity collisions occurred between two fully forme

21 extraction), added phosphate eliminated the low velocity component.

22 interior undergoes significant stirring with low-velocity conduits along its edges and down-welling n

23 Low velocities continue downward to the mantle transitio

24 Bubbles at very low velocities, corresponding to capillary numbers Ca <

25 cta persistently imprint Phobos with linear, low-velocity crater chains (catenae) that match the geom

26 es between the protocluster galaxies and has low velocity dispersion, indicating that it is part of a

27 sHMM Qdot-actin velocity histogram contains low-velocity events corresponding to actin translation i

28 e seismic experiments, that reveals a strong low-velocity feature beneath the subducting Juan de Fuca

29 e geodynamic arguments, we propose that this low-velocity feature is the accumulation of material fro

30 ved wave intensity analysis using a pressure-low velocity guidewire at baseline and again 30 minutes

31 over the nature of geophysically recognized low-velocity-high-conductivity zones (LV-HCZs) within th

32 could be either exogenic, from carbon-rich, low-velocity impactors, or endogenic, from freshly expos

33 The low-velocity layer (about 8 kilometers thick) dips 30 de

34 The low-velocity layer (LVL) atop the 410-km discontinuity h

35 ower mantle is a plausible candidate for the low-velocity layer because of its broad thin extent.

36 e relevant only to regions of low oxygen and low velocity, leaving a wide gap in our understanding of

37 The recent discovery of a low-velocity, low-Q zone with a width of 50-200 m reachi

38 rger than that in the isometric state at the low velocities (<0.5 L(0) s(1)) but decreased to below t

39 For low-velocity (<1 m/s) off-center collisions, mixing time

40 Low velocities near the axis are probably caused by part

41 ulations indicated that this was a result of low-velocity nearshore currents promoting the retention

42 dynes/cm2, RO+ T cells rolled extensively at low velocity on both CHO-P and CHO-E monolayers and VCAM

43 ropagate under physiological conditions at a low velocity over limited distances.

44 elocity phase of shortening and a subsequent low velocity phase of shortening.

45 NEM-S1 from the treated fibres restored the low-velocity phase of shortening and returned low-veloci

46 d fibres with 5 microM NEM-S1 eliminated the low-velocity phase of shortening but had no effect on th

47 f unloaded shortening velocity (V(o)) in the low-velocity phase was investigated by varying the level

48 o fewer, undulating but vertically coherent, low-velocity plumelike features, which appear rooted in

49 al arteries to the relatively low-oxygen and low-velocity postcapillary venules.

50 he notion that many hot spots originate in a low-velocity, probably partially molten layer at the cor

51 The Earth's lowermost mantle large low velocity provinces are accompanied by small-scale ul

52 Large low velocity provinces are hypothesized to be caused by

53 In contrast to previous work, we explore a low-velocity regime described by the three-dimensional B

54 nergy of guided waves is concentrated at the low velocity region near the stopband.

55 re can be found at the base of the two broad low-velocity regions under the Pacific Ocean and under A

56 Large low-velocity seismic anomalies have been detected in the

57 nwards (towards the center of the A-band) at low velocity shortening (around 0.9 T0): their dispersio

58 h-velocity shortening followed by a phase of low-velocity shortening.

59 three concentrated locations of anomalously low velocities spaced about 250 kilometres apart.

60 At low velocity, the slope of the relation between the fric

61 ets at shear rates up to 6,300 s-1 mediating low velocity translocation but not stable attachment; in

62 mitochondria docked to the axonal framework (low velocity transport [LVT]).

63 atic injury in patients who have experienced low-velocity trauma and have acute head and/or cervical

64 iber diameter d approximately 0.1 microm) at low velocity (U = 1.6 +/- 0.6 cmxs(-1), mean +/- SD) and

65 tomography reveals intense large-scale hot (low-velocity) upwelling features not explicitly predicte

66 The effect of NEM-S1 to increase low-velocity V(o) can be explained in terms of a model i

67 ow-velocity phase of shortening and returned low-velocity V(o) to pre-treatment values.

68 Simulations yield low-velocity values for the Young's modulus of 6.0 GPa.

69 ed matter obeys in the biologically relevant low-velocity viscous regime a simple law: the friction f

70 One is defined as a low-velocity viscous regime inherent to a noncovalent, p

71 of the PKP phase were used to study an ultra-low velocity zone (ULVZ) near the core-mantle boundary b

72 c interplay between plate-driven flow in the low-velocity zone and active influx of low-rigidity mate

73 n the upwelling mantle, explains the oceanic low-velocity zone and the electrical conductivity struct

74 We interpret the low-velocity zone as a compositional anomaly, possibly d

75 This low-velocity zone has a thickness that varies from 20 to

76 We image a large low-velocity zone in the crust, consisting of a shallow

77 The presence of the midcrustal low-velocity zone in the north implies that a partially

78 sequently, the mantle geotherm is hot if the low-velocity zone is anhydrous, but cold if hydrated.

79 neath the southern Lhasa block, a midcrustal low-velocity zone is revealed by inversion of receiver f

80 o the south beneath the Tethyan Himalaya, no low-velocity zone was observed.

81 -waveform tomography, we reveal an expansive low-velocity zone, which we interpret as a possible hot

82 We find a low-velocity zone, with a shear-wave velocity drop of 5%

83 epth, which extends below the well-developed low-velocity zone.

84 If the ultra-low-velocity zones are composed of Fe-enriched silicate

85 rface of Earth and the distribution of ultra-low-velocity zones at the base of the mantle has about a

86 an explanation to the low-velocity and ultra-low-velocity zones.