ライフサイエンスコーパス: fault

1 ugh a rigid and low-permeability rock to the fault.

2 hanical parameters of the actively deforming fault.

3 ric geometry of the north-dipping Centennial fault.

4 nd geometry of a well-known offshore capable fault.

5 ace and trench-parallel motion on the sliver fault.

6 y by a ~40-45 degrees , east-dipping, normal fault.

7 e energy-dissipation-rate along the slipping fault.

8 planar geometry of the Main Himalayan Thrust fault.

9 s ascending fluids pressurize and weaken the fault.

10 quare site adjacent to a subsurface stacking fault.

11 increase the fault strength of the megasplay fault.

12 field assisted self-healing (eFASH) of open faults.

13 ries (GBs) and Ruddlesden-Popper (RP) planar faults.

14 ters, magma intrusion pathways and inherited faults.

15 agate across negatively stressed portions of faults.

16 in character to those observed along natural faults.

17 multiscale network of interlaced orthogonal faults.

18 ce of vertical CO(2) leakage linked to known faults.

19 xt generation of analyses of earthquakes and faults.

20 earthquakes rarely rupture nearest neighbor faults.

21 that encompasses the trace of nearby active faults.

22 through nucleation of steps along the planar faults.

23 ve therapies exist that target these genetic faults.

24 xis, core complexes, detachment or transform faults.

25 ent highs with growth geometry against these faults.

26 slow, aseismic slip on preexisting, shallow faults.

27 table and unstable sliding of landslides and faults.

28 eismic studies of fast-moving plate-boundary faults.

29 al dislocation in between these two stacking faults.

30 uid pressure data from active plate-bounding faults.

31 s determined by the friction evolution along faults.

32 aseismic transient slip on oceanic transform faults.

33 dated by frictional slip on many preexisting faults.

34 b-Cenozoic unconformity, bounded by two tear faults.

35 le Basin opened after this time along normal faults.

36 pressure and unsteady fluid migration along faults.

37 increase in geothermal gradient over crustal faults.

38 emporal variations in the mechanical work of faulting.

39 ale deformation over broad regions of active faulting.

40 ion of middle/lower crust through detachment faulting.

41 h the remaining time lost due to engineering faults (0.6% of the time), CO(2) supply issues (0.6%) or

42 , the alternate development of perpendicular faults accommodates synchronous bi-directional and mutua

43 ble of explaining the frictional behavior of faults, across the full range of slip velocities (10(-9)

44 uid flow systems in the region and transform faults act as an additional major pathway for fluid circ

45 of the Mojave block and a re-distribution of fault activity since the Pleistocene.

46 rce increasing the hydraulic conductivity in faults allowing organisms to create ecosystems in the de

47 at the Coso volcanic area and at the Garlock Fault and brought some neighbouring faults closer to fai

48 deposits shows leakage varies along a single fault and that individual seeps have lifespans of up to

49 ent initiated on a right-lateral NW striking fault and then ruptured a left-lateral fault to the surf

50 It ruptured a previously unmapped fault and triggered aftershocks along a complex conjugat

51 es are recognised, linked by transpressional faulting and compressional strike-slip relay ramps, as w

52 Faulting and earthquakes occur extensively along the fla

53 d cages and as well as to twinning, stacking faults and antiphase boundary defects.

54 s initiate seismicity on critically stressed faults and Coulomb static stress transfer modeling revea

55 unattended plants, soft sensors could expose faults and failures to the operator.

56 ilure in earthquakes is not the same for all faults and is dependent on the geometry of the fault/she

57 erved through nucleation of a pair of planar faults and lateral growth of the twins occurs through nu

58 that host active swarms on oceanic transform faults and provides candidates for future seafloor geode

59 ectron microscope, it is found that stacking faults and rotational disorders in multilayered 2D cryst

60 ecific uncertainty such as hidden/undetected faults and stress regime.

61 tions for phyllosilicate bearing seismogenic faults and subduction zones.

62 understand the kinematics of basin bounding faults and their role in accommodating proposed right-la

63 esults demonstrate that the surface stacking faults and twin defects increase CO binding energy, lead

64 y capability with strong tolerances to input faults and variations, which shows the feasibility of us

65 ction interface, the non-rupture of the Hope fault, and slow apparent rupture speed.

66 uctures, a corrugated and grooved detachment fault, and subdetachment deformation involving crustal-s

67 e selection of dislocation pathways in slip, faulting, and twinning, and increases the lattice fricti

68 geneity due to permeable conduits and normal faults, and to recharge from rivers during sea level low

69 vely two-dimensional (2D) models for general fault architecture.

70 n is strongly controlled by 3D variations in fault architecture.

71 These faults are associated with prominent topographic feature

72 ploit ancient faults, but not all intraplate faults are equally active.

73 These fossil seismogenic faults are rarely >15 m in length, yet record single-eve

74 Longer paleoseismic records for intraplate faults are required both to better quantify their earthq

75 Conversely, where faults are stress-loaded by across-strike fault interact

76 recurrence for a system of 25 active normal faults arranged predominantly along strike from each oth

77 ust is an on-land analog of the modern splay fault at shallow depths (~ 8 km) in the Nankai Trough.

78 A system of tear faults at a high angle to the orogen is spatially locali

79 enters in silicon carbide as a near-stacking fault axial divacancy and show how this model explains t

80 find that the change of normal stress on the fault before the earthquake is not uniform but increases

81 most reliable representations of subsurface fault behavior, as they produce geologically reasonable

82 nical properties of the shallow crust affect fault behavior.

83 formation, including the 8-meter uplift of a fault-bounded block.

84 ture periodically distributed basal stacking faults (BSFs), which facilitates the study of the influe

85 nced by the presence of basal-plane stacking faults (BSFs).

86 Shear heating may occur within the fault but is not required to explain our observations.

87 c plate boundaries generally exploit ancient faults, but not all intraplate faults are equally active

88 poroelastic energy and pore pressure along a fault can nucleate seismic events larger than M(w)3 even

89 Faults can slip not only episodically during earthquakes

90 Garlock Fault and brought some neighbouring faults closer to failure.

91 f CO(2) leakage above a naturally occurring, faulted, CO(2) reservoir in Arizona, USA.

92 flow front offset along a first-order Riedel fault complex records slip at ~3.8 mm a(-1), which may b

93 First-order en-echelon Riedel fault complexes are recognised, linked by transpressiona

94 and plastic yielding than to the presence of fault compliant zones (i.e., regions surrounding faults

95 plates is off-centered from the San Andreas fault, concentrated in a region that encompasses the tra

96 e elastic half-space modelling on non-planar faults, constrained by the geology and geomorphology of

97 Thus, sliver faults could be responsible for the downdip end of the s

98 h rate, whether defined as all crashes or at-fault crashes only (all p > 0.05).

99 .28, 95% CI: 1.01-1.63, respectively) and at-fault crashes only (RR: 1.50, 95% CI: 1.16-1.93; RR: 1.3

100 on and stress concentrations induced by deep fault creep.

101 ndicate a strong correlation between crustal faults, crustal highs and fluid accumulations in the ove

102 etric data, we map tectonic features such as faults, crustal highs, and indicators of fluid flow proc

103 id injection are usually assumed to occur on faults destabilized by increased pore-fluid pressures.

104 Oceanic transform faults display a unique combination of seismic and aseis

105 d illuminate the subsurface stratigraphy and faults down to ~1200 m, showing that the basin is a half

106 lude that stress perturbation on prestressed faults due to pore-pressure diffusion, enhanced by poroe

107 riments along granite and diorite laboratory faults, during which the faults were subjected to contro

108 actor contributing to this phenomenon is the faults' dynamic friction, which may be reduced during ea

109 In the context of crustal faulting dynamics, these results suggest that evolving r

110 preferentially during low tide, when normal faulting earthquakes should be inhibited.

111 of vertical motions and that of other normal faulting earthquakes, and (b) for the first time model t

112 face-centred cubic metals with low stacking fault energies when tuning the GB structure, external ge

113 producing a wide range of generalized planar fault energies.

114 to enhancements in ductility in low stacking fault energy (SFE) alloys, however to achieve an unconve

115 such order give rise to both higher stacking-fault energy and hardness.

116 Here, the stacking fault energy in the high-entropy nanotwinned crystalline

117 s in composition and an increase in stacking-fault energy, leading to higher yield strength without c

118 Faults exhibit a gamut of slip styles from stable slidin

119 Where only one fault exists across strike, stress-loading is dominated

120 gins (ophiolites), and along the seafloor as faulting exposes this mantle-derived material to circula

121 Large continental faults extend for thousands of kilometres to form bounda

122 vated in plastic deformation of low stacking-fault face-centered cubic (Fcc) metals but rarely found

123 The inner core has a monotwinned/stacking-faulted face-centered-cubic (fcc) structure.

124 e lavas; a tabula rasa recording innumerable fault features displayed in exquisite detail.

125 iations in fault-normal stress, which affect fault friction.

126 the up-dip portion (shallower depth) of the fault from the hypocenter and decreases in the down-dip

127 al structures (extensional cracks and normal faults) generated during the post-seismic period create

128 d viscosity (eta), co-seismic slip-rate (V), fault geometry (L/H(0)(2)) and earthquake nucleation dep

129 This complex fault geometry persists over the entire seismogenic dept

130 Similar study of intraplate faults has been limited until now, because intraplate ea

131 Our results show that multiple faults have hosted earthquakes with displacement >= 10 m

132 tion intersection between the Husavik-Flatey Fault (HFF) dextral transform and rifting in the Norther

133 The electric field appearing in the open fault in a current carrying interconnect polarizes the c

134 , despite the existence of a stable stacking fault in the basal plane gamma surface, the dislocation

135 Understanding the approach to faulting in continental rocks is critical for identifyin

136 ing) in eastern North America to strike-slip faulting in the mid-continent to predominantly extension

137 ore-pressure accumulation along pre-existing faults in deep basement contribute to recent occurrence

138 rmal maturity indicators to identify seismic faults in drill core recovered from the Japan Trench sub

139 Open circuit faults in electronic systems are a common failure mechan

140 is problem several methods to self heal open faults in real time have been investigated.

141 Genetic faults in several components of the nuclear factor-kappa

142 aid by a kinematically consistent network of faults in the brittle crust.

143 ne linking the Centennial and Lima Reservoir faults in the Centennial Valley.

144 ction plays a key role in how ruptures unzip faults in the Earth's crust and release waves that cause

145 ismic slip along 40-60 degrees planar normal faults in the elastic upper crust, followed by postseism

146 etwork that lead to cancer are abstracted as faults in the equivalent circuit and the Boolean circuit

147 from compression (strike-slip and/or reverse faulting) in eastern North America to strike-slip faulti

148 er the present-day trace of the MFT as blind faults inaccessible to trenching, and that paleoseismic

149 ive earthquakes often propagate along thrust faults including megathrusts.

150 rt of the accommodation zone and seismogenic faults including the Lima Reservoir fault that has well-

151 eal surface ruptures along at least 12 major faults, including possible slip along the southern Hikur

152 st hinders efforts to mitigate hazards where faults increasingly intersect with the expanding global

153 ulations reveal that neither of these planar faults induce deep defect levels, but their Br-deficient

154 damage around existing locked or future main faults influences the localization process that culminat

155 ional strain versus across- and along-strike fault interaction.

156 re faults are stress-loaded by across-strike fault interactions, fault planes have more irregular str

157 n, which explains the presence of the normal faults interpreted in 3-D seismic profiles collected fro

158 and a working interpretation that identifies fault inversion, and an oblique, anticlinal accommodatio

159 The fault is interpreted as the southwestern margin of an in

160 A blind thrust fault is interpreted in the subsurface, above the sub-Ce

161 data, finite element models indicate shallow faulting is more sensitive to lithologic layering and pl

162 he atmosphere via leakage through geological faults is a potential high impact risk to CO(2) storage

163 me slip at shallow depths on subduction zone faults is a primary contributor to tsunami generation by

164 Coulomb pre-stress calculated for non-planar faults is an ignored yet vital factor for earthquake tri

165 ions show that the correction of 2D stacking faults is triggered by the ejection of Mo atoms in mirro

166 of the earthquake with the Newport-Inglewood fault; it further illuminates the concentration of sever

167 During earthquake propagation, geologic faults lose their strength, then strengthen as slip slow

168 mic slip propagation is facilitated by along-fault low dynamic frictional resistance, which is contro

169 rincipally a strike-slip plate boundary, the faulted margins of the Gulf display largely dip-slip ext

170 le fluids are escaping along a crustal-scale fault marked by clusters of non-volcanic tremors directl

171 The predicted shaking for a 25-km-long fault matches the intensity distribution, with an indica

172 uakes and interseismic loading on non-planar faults) may explain this, evidenced by study of a 667-ye

173 t; however, the effect of fluid viscosity on fault mechanics is mainly conjectured by theoretical mod

174 t the energy balance of all processes during fault movement, we present a framework that reconciles t

175 astic deformation by forming at the stacking-fault network boundaries in the fcc phase, serving as th

176 with regional stress estimates and a crustal fault network geometry inferred from seismic and geodeti

177 facilitate the construction of the stacking-fault networks to provide nucleation sites for the hcp p

178 result in stable three-dimensional stacking-fault networks.

179 e free surface leads to sudden variations in fault-normal stress, which affect fault friction.

180 nt of Sierra de Santa Catarina-where surface faulting occurs.

181 and is the same for the 2 optimal, conjugate fault orientations suggested for Oklahoma.

182 slip rate of 4.5-9.0 mm.yr(-1) on the master fault over the past ~610 ka and an uplift/subsidence rat

183 lly perpendicular extension, giving the same fault pattern observed in the Barents Sea rift-shear mar

184 Twin detachment faults penetrating to the depth of 13 +/- 2 km below the

185 seismic period, when healing/sealing reduces fault permeability, and is released after earthquakes en

186 -loaded by across-strike fault interactions, fault planes have more irregular stress patterns and int

187 s through slip on underlying shear zones and fault planes have spatially smooth stress with predomina

188 likely influence early rift sedimentary and faulting processes, potentially including syn-rift strat

189 ubduction interface trenchward of the sliver fault, promoting fast-slip seismogenic rupture behavior.

190 These slip styles are affected by the fault properties, e.g., weakening or strengthening, and

191 We propose that the sliver fault provides a natural pathway for buoyant fluids atte

192 acial time, although with transform-affinity faults reactivated to accommodate rift extension and tra

193 n points and the critical fluid pressure for fault reactivation can be used for a better prediction o

194 nductivity anomalies along the strike of the fault recognized previously correlated up dip with the s

195 The faults record the subsurface propagation of the Main Him

196 ear grabens coupled with minor perpendicular faults, resulting in the triple junctions of grabens obs

197 The deep subvertical detachment fault roots on the plate boundary, marked by a thermal a

198 ed materials is known as rotational stacking fault (RSF), but the coexistence of multiple RSFs with d

199 l strike-slip displacement, characterise the fault segmentation and demonstrate that AIFS is the sour

200 d to assess earthquake potential on specific fault segments.

201 tiated through the formation of two stacking faults separated by a single atomic layer, and proceeded

202 Alternatively, multiple fault sets have been proposed to develop simultaneously

203 e blocks, pristine pseudotachylytes decorate fault sets that link adjacent or intersecting shear zone

204 While stacking faults (SFs) contribute to strengthening by impeding dis

205 bits a tendency to segregate to the stacking faults (SFs).

206 stress there, which leads to an increase of fault shear strength and allows more elastic strain ener

207 an extent explainable, given constraints on fault/shear-zone interaction and the build-up and releas

208 ults and is dependent on the geometry of the fault/shear-zone system.

209 ations supporting maps of capable non-planar faults should not be ignored when attempting to identify

210 gery, coupled with 120 field measurements of fault slip directions and opening amounts, made possible

211 hesized that the weakening phenomenon during fault slip may be activated by thermal pressurization of

212 ents to verify the relation between aseismic fault slip, earthquake swarms, and fault zone hydromecha

213 r this delay is important for simulations of fault slip, ground motion, and associated tsunami excita

214 inated by either co- or post-seismic shallow fault slip.

215 magnitude (M (w)) 6.9] produced ~5 meters of fault slip.

216 Poor knowledge of how faults slip and distribute deformation in the shallow cr

217 al cracks contributes little to increase the fault strength of the megasplay fault.

218 fluid pressure decrease, and (ii) the degree fault strength recovery by the extension crack formation

219 us reducing the pore pressure and increasing fault strength.

220 e fluids control effective normal stress and fault strength.

221 umulation of elastic strain energy until the faulting strength was overcome, thereby generating the L

222 ess at the studied wellbore is in the normal faulting stress regime within the Tarim Basin rather tha

223 resistivity structure surrounding the sliver fault suggests that SSEs and swarms of earthquakes occur

224 dip with the surface trace of a major active fault support the hypothesis.

225 ructure in its initial-stage, the Al-Idrissi Fault System (AIFS), in the Alboran Sea.

226 rogeneity in Coulomb pre-stresses across the fault system is >+/-50 bars, whereas coseismic CST is <+

227 e derived fluids, suggesting that the active fault system is deep-seated.

228 We propose that the complex fault system operates at low apparent friction thanks to

229 ot springs, and bedrock samples from a major fault system that separates regional-scale blocks of acc

230 ception and growth of a young plate boundary fault system.

231 akes along the Newport-Inglewood/Rose Canyon fault system.

232 ggered aftershocks along a complex conjugate fault system.

233 at swarms and SSEs are occurring on a sliver fault that allows the oblique convergence to be partitio

234 smogenic faults including the Lima Reservoir fault that has well-expressed Holocene surface ruptures

235 orly understood effect of energy-flux to the fault that should equal or exceed the energy-dissipation

236 stresses, producing Coulomb stresses on the faults that are opposite in sign to those produced by th

237 arthquake recurrence intervals of intraplate faults therefore are poorly understood.

238 In natural faults, this nanopowder crystallizes to quartz over 10s-

239 iking fault and then ruptured a left-lateral fault to the surface.

240 We use analogue models of normal faults to demonstrate that, without the influence of pre

241 Whether the stress-loading of faults to failure in earthquakes appears to be random or

242 e accuracy remains unchanged, and has better fault tolerance and scalability.

243 o modes (MZMs) offers an approach to achieve fault tolerance by encoding quantum information in the n

244 elp to speed up quantum circuits and achieve fault tolerance in trapped-ion quantum computers.

245 l as substantial physical qubits, to realize fault tolerance via quantum error correction(2,3).

246 e demonstrated two-qubit fidelities near the fault-tolerance threshold(6) have been in superconductor

247 structure and circuit simulation is stable, fault tolerant and efficient, which is a useful compleme

248 A new scalable and fault tolerant storage backend, Application Programming

249 d by noise from multiplying and spreading, a fault-tolerant computational architecture is required.

250 y, quantum gate parallelism is essential for fault-tolerant error correction of qubits that suffer fr

251 Significant advances have been made towards fault-tolerant operation of silicon spin qubits, with si

252 de variety of noise processes and facilitate fault-tolerant quantum computation.

253 ng codes that, with higher squeezing, enable fault-tolerant quantum computation.

254 atistics and the realization of braiding for fault-tolerant quantum computation.

255 While fully fault-tolerant quantum computers are not yet realized, t

256 ications for dissipationless electronics and fault-tolerant quantum computers(4,5).

257 are expected to be ideal building blocks for fault-tolerant quantum computing(1,2).

258 ical MBQC in superconducting circuits toward fault-tolerant quantum computing.

259 , quantum error correction creates a path to fault-tolerant quantum information processing(4).

260 hem is a key requirement for large-scale and fault-tolerant quantum information processors.

261 ing radiation will be critical for realizing fault-tolerant superconducting quantum computers.

262 w kilometers from the major regional Garlock fault, triggering shallow creep and a substantial earthq

263 ht explain observations of late interseismic fault unlocking, slow slip and creep transients, swarm s

264 ure distribution, geologists have documented fault valving behavior, that is, cyclic changes in press

265 Here we quantify fault valving through 2-D antiplane shear simulations of

266 One stacking fault with a fault vector b/6[110] and low mobility contributes minim

267 InSAR is transforming our understanding of faults, volcanoes and ground stability and increasingly

268 compressive force introduced by a ramp/flat fault was suggested as its origin of formation; however,

269 nerally believed that earthquakes occur when faults weaken with increasing slip rates.

270 increase and earthquake interactions lead to fault weakening and ultimately triggering larger earthqu

271 diorite laboratory faults, during which the faults were subjected to controlled energy-flux, and res

272 to circumvent nearest-neighbour along-strike faults where coseismic CST is greatest.

273 ong a locked section of the 2013 seismogenic fault, which caused the accumulation of elastic strain e

274 e partitioned into coupled systems of normal faults, which display geometries commonly observed in te

275 twin boundaries (TBs) and multiple stacking faults, which lead to low overpotentials for methane (CH

276 t the pore pressure and slip history imply a fault whose strength is the product of a slip-weakening

277 Our results indicate slip on the capable fault with a dip to the east of 70 degrees and 5 m dip-s

278 One stacking fault with a fault vector b/6[110] and low mobility cont

279 migration within a shallower section of the fault with fundamentally different mechanical properties

280 ons of earthquake sequences on a strike-slip fault with rate-and-state friction, upward Darcy flow al

281 sisting of a graphene monolayer rotationally faulted with respect to a Bernal-stacked bilayer to real

282 a-caldera eruption at Ambrym preceded normal faulting with >2 m of associated uplift along the easter

283 te, rather than simultaneous, development of faults with different trends.

284 Complex patterns of normal faults with multiple orientations and/or highly curved s

285 t compliant zones (i.e., regions surrounding faults with reduced stiffness).

286 atural CO(2) seeps along the Ntlakwe-Bongwan fault within KwaZulu-Natal, South Africa, have C-He isot

287 that fluids are naturally injected into the fault zone from below and diffuse through strike-paralle

288 ng with a deep-learning algorithm to image a fault zone hosting a 4-year-long swarm in southern Calif

289 aseismic fault slip, earthquake swarms, and fault zone hydromechanical properties.

290 magnitude earthquakes a step-over along the fault zone results in the vertical displacement of an ap

291 ndwater withdrawals in the Edwards (Balcones Fault Zone) Aquifer, where listed species are found.

292 riction, upward Darcy flow along a permeable fault zone, and permeability evolution.

293 locations of the topographical extreme belt, fault zone, seismic belt, and dry valleys.

294 uakes occur due to high fluid content in the fault zone.

295 a large fracture cluster that evolves into a fault zone.

296 Fault-zone fluids control effective normal stress and fa

297 ides important insights into the geometry of fault zones at depth, foreshock behavior and nucleation

298 Fluids are pervasive in fault zones cutting the Earth's crust; however, the effe

299 eriments performed at a decameter scale into fault zones in limestone and shale formations.

300 uake wavefield identified multiple submarine fault zones.