ライフサイエンスコーパス: low-velocity

1 w force, high velocity; running: high force, low velocity).

2 or at high velocities to brittle response at low velocities.

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

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

5 Its two lenticular lobes suggest low-velocity accumulation of numerous smaller planetesim

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

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

8 The seismic low velocities and the high electrical conductivities of

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

10 regions containing low shear rate, high OSI, low velocity, and flow stasis in comparison to subjects

11 g shear rate, oscillatory shear index (OSI), low velocity, and flow stasis were calculated and compar

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

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

14 anomalies rather than the previously assumed low-velocity anomalies.

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

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

17 The horizontally elongated low-velocity anomaly is also featured by a distinctive p

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

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

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

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

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

23 Low-velocity ballistic trauma to the inferior sclera cre

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

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

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

27 ixed layer properties in relatively warm and low-velocity cavity environments.

28 to surface wave energy trapped in this local low-velocity channel.

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

30 that Selam likely formed through a series of low-velocity collisions of similarly sized moonlets that

31 We interpret the low-velocity columns as damaged zones caused by seamount

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

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

34 ights the presence of several separate broad low-velocity conduits anchored at the core-mantle bounda

35 Low velocities continue downward to the mantle transitio

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

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

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

39 s and large globular clusters(2-6), and very low velocity dispersions that indicate little or no dark

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

41 supershear segment aligns with a ~2-km-thick low-velocity fault zone exhibiting ~45% shear wave speed

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

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

44 s in this area are sensitive to small-vessel low velocity flow without use of intravenous contrast ag

45 We find that at low velocities, friction is controlled by hydrodynamic f

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

47 ilize the head, in contrast to rats that use low-velocity head movements to scan the environment as t

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

49 le, flexure, compression, in-plane shear and low velocity impact response.

50 s exhibited superior energy absorption under low velocity impact, at energy levels 15-60 J.

51 operties are experimentally assessed through low-velocity impact (1.54 m/s) and quasi-static compress

52 ite, majorite, and albitic jadeite; later, a low-velocity impact formed fractures and filled them wit

53 asi-static compression and 34% and 74% under low-velocity impact, respectively.

54 cosity and energy dissipation in response to low-velocity impact.

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

56 rtificial AE sources (Pencil lead break) and low-velocity impacts.

57 e find that high attenuation correlates with low velocity, indicating a thermal origin, in agreement

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

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

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

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

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

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

64 of the continent, highlighted by 1) shallow low velocities (<3.2 km/s) well correlated with the loca

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

66 ca, which hinders the formation of a typical low-velocity mantle wedge and arc volcanoes.

67 ll imaged as high-velocity features, where a low-velocity mantle wedge exists and demonstrate a stron

68 ent with pebble cloud collapse followed by a low-velocity merger of its two lobes.

69 Low velocities near the axis are probably caused by part

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

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

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

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

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

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

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

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

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

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

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

81 Large low velocity provinces are hypothesized to be caused by

82 The two "large low velocity provinces" (LLVPs) are broad, low seismic w

83 h low seismic velocities, known as the large low-velocity provinces (LLVPs), in the lowermost mantle(

84 Seismically observed "large low-velocity provinces" (LLVPs) are thought to have resu

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

86 e proposed, where the relative extent of the low velocity region is made tunable by exploiting a two-

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

88 tively large particles from experiencing the low velocity region near the walls of a pressure-driven

89 rovide direct constraints on the geometry of low velocity regions beneath volcanoes despite having a

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

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

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

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

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

95 In particular, the low-velocity stopping range, that features the largest m

96 We interpret the low-velocity structure as the possible source of Mid-Oce

97 rated into the mantle, they would form dense low-velocity structures above the CMB, which may account

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

99 the MMR with a melt fraction of ~4-11% and a low-velocity throat beneath the eastern caldera wall con

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

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

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

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

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

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

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

107 n the middle Lhasa Terrane has exceptionally low velocity (V(p) < 6.7 km/s) throughout the whole 80 k

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

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

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

111 vicinity and within the turbine's turbulent, low-velocity wake, indicating avoidance behaviour.

112 ex shallow bathymetry of the area acted as a low-velocity wave trap, capturing tsunami for more than

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

114 Results reveal the presence of a broad low velocity zone between 40 and 80 km depth affecting m

115 s km-scale shrinkage or movement of an ultra-low velocity zone near the core-mantle boundary, and (2)

116 istent with a plume rooted in a lower mantle low-velocity zone also sampling primordial components.

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

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

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

120 We found a structure compatible with a low-velocity zone associated with a thermal lithosphere

121 bove stacks of lava flows, we find a seismic low-velocity zone at about 30 to 75 m depth that we inte

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

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

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

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

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

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

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

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

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

131 These findings suggest that ultra-low velocity zones are deformed as partially molten mate

132 reme heterogeneities yet observed are 'Ultra-Low Velocity Zones' (ULVZ).

133 ere, with detailed mappings of intra-crustal low-velocity zones and crust-mantle discontinuity in the

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

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

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