ライフサイエンスコーパス: crust

1 tems emplaced at the base of the continental crust.

2 ct throughout the quartz-bearing continental crust.

3 bundance of main group metals in the Earth's crust.

4 chemosynthetic activity within igneous ocean crust.

5 eanic crust subducts beneath the continental crust.

6 leased from the mantle and subducted oceanic crust.

7 ks, which are building blocks of continental crust.

8 cgeAB, encode the protein components of the crust.

9 ssociated with ascent through over-thickened crust.

10 e the observed geophysical properties of the crust.

11 butes to anomalous enrichments of CSE in the crust.

12 ization of cooling magma stalled beneath the crust.

13 isotropy has never been detected in cratonic crust.

14 luence the transfer of fluids in the Earth's crust.

15 s that penetrate kilometers into the Earth's crust.

16 l distribution, and longevity of melt in the crust.

17 ent and typically occur near the base of the crust.

18 differences between Indian and Pacific Ocean crust.

19 an atmosphere and also deeper in the porous crust.

20 higher volcanic productivity and thicker arc crust.

21 ndense outer coat striations, but retain the crust.

22 dence concerning the nature of Earth's first crust.

23 chemical and isotopic composition of oceanic crust.

24 2-rich volatile phase while it traversed the crust.

25 ustal-scale outline of the subducting Indian crust.

26 te a long-term accumulation of stress in the crust.

27 ted in a strengthened dough and firmer pizza crust.

28 production and consumption in young oceanic crust.

29 y modified in hydrothermally altered oceanic crust.

30 rmal exchange between seawater and the ocean crust.

31 linked to the age of the subducting oceanic crust.

32 n magmas that incorporate felsic continental crust.

33 ce of a "deep, hot biosphere" in the Earth's crust.

34 ma bodies several kilometers deep within the crust.

35 gin of a broad conductive region in the deep crust.

36 osed along a structure that excised 25 km of crust.

37 meteoric waters during their cooling in the crust.

38 horizontal advance of the subducting Indian crust.

39 ength heterogeneity of the Asian continental crust.

40 ear the base of thick, plateau-like basaltic crust.

41 a critical part in the sequestration of the crust.

42 o consider magmatic processes throughout the crust.

43 y buoyant melt migration to form the oceanic crust.

44 consistent network of faults in the brittle crust.

45 kali components extracted from the subducted crust.

46 cur during magma ascent through a chondritic crust.

47 nomalous) (182)W characteristic of subducted crust.

48 proposed to be related to subducted oceanic crust.

49 electrodense outer coat and a more external crust.

50 om melts of carbonate-rich subducted oceanic crust.

51 ng minerals that make up most of the Earth's crust.

52 forming some 5 million km(2) new continental crust.

53 e, in the deep ocean, and within the Earth's crust.

54 t the geological processes that form oceanic crust.

55 in mantle domains least modified by recycled crust.

56 ry for proper encasement of the spore by the crust.

57 inked by structures that transect the entire crust.

58 ocal clastic materials and upper continental crust.

59 ced by the outermost layer of the spore, the crust.

60 of the formation and evolution of planetary crusts.

61 ered on the low Nb/Ta of Earth's continental crust (11-13) compared to basalts (15-16).

62 It is denser (5.15 g/cm(3)) than Earth's crust (~2.7 g/cm(3)) and is expected to accumulate at th

63 roducing magmas that ascend to form basaltic crust 6 to 7 kilometers thick.

64 ry, indicating that the North China cratonic crust acts as a strong resistance to the northward growt

65 ate and mechanical properties of the shallow crust affect fault behavior.

66 During convergence, a weaker Asian crust allows strain far north within the upper plate, wh

67 ermine the velocities and density of oceanic crust along different mantle geotherms.

68 ial diversity in Mediterranean semiarid soil crusts along an aridity gradient by using next-generatio

69 Appealing crust and crumb colour and good sensory characteristics

70 rphic core complexes, boudinage of the upper crust and exhumation of middle/lower crust through detac

71 hich is mainly composed of Neoarchean felsic crust and forms the nucleus of the Northeastern Superior

72 is the most abundant actinide in the Earth's crust and has universally been considered one of the mos

73 Conversely, relatively buoyant mafic crust and hotter geothermal gradients on Earth reduced t

74 Parallel fast axes in the crust and mantle indicate coupled crust-mantle evolution

75 suggested that multiphase deformation of the crust and mantle lithosphere leads to the formation of d

76 ifferent potential fluid sources (sediments, crust and mantle lithosphere) and tracing fluids from th

77 heric mantle as well as the coupling between crust and mantle lithosphere, which may be inferred by s

78 uilding block of major mineral phases in the crust and mantle of terrestrial planets (1-10 M(E)).

79 te the impactor mass accreted into the lunar crust and mantle over their histories.

80 bian plate from in situ Gulf of Oman oceanic crust and mantle presently subducting northwards beneath

81 that, to match the HSE budgets of the lunar crust and mantle(5,6), the retention of HSEs should have

82 flow is powered by radioactive decays in the crust and mantle.

83 ntributed these volatile elements to Earth's crust and mantle.

84 magma, earthquakes, formation of continental crust and mineral resources.

85 microbial biosphere extends down through the crust and much of the subsurface, including those microb

86 in how ruptures unzip faults in the Earth's crust and release waves that cause destructive shaking.

87 constraint on the flux of K between oceanic crust and seawater.

88 standing of how strain is distributed in the crust and the ability to precisely detect millimeter-sca

89 ism for the generation of voluminous silicic crust and the development of Cordilleran plateaus remain

90 cannot distinguish between anisotropy in the crust and the mantle.

91 red to be the interface between the magnetic crust and the non-magnetic mantle(1).

92 g in a wide variety of rock types in Earth's crust and upper mantle.

93 < 0.05) higher specific volume, but lighter crust and weaker aroma (lower amounts of Maillard reacti

94 se any significant textural changes in pizza crusts and partial replacement by KCl resulted in a stre

95 action of poly-metallic nodules, cobalt-rich crusts and sulphide deposits from the ocean floor.

96 of the martian mid-to-low latitudes (average crust) and flows in northwest Elysium.

97 ich to identify ancient fragments of oceanic crust, and as a constraint on the flux of K between ocea

98 n plate tectonics and a paucity of subaerial crust, and consequently lacking an efficient mechanism t

99 with moderate enrichment of recycled oceanic crust, and mid-mantle discontinuities can be explained b

100 ast 4.5 billion years formed the continental crust, and produced at least one complementary melt-depl

101 derived from metasediments, altered oceanic crust, and serpentinite have delta(34)S values of approx

102 ductivity zones (LV-HCZs) within the Tibetan crust, and their role in models for the development of t

103 the industrial sections; cutting, shivering/crusting, and stitching were the principal contributors

104 belonging to built heritage (mortars, black crusts, and calcium carbonate formations).

105 he burial and metamorphism of hydrated mafic crusts, and calculate mineral transition-induced bulk-de

106 Thus, unlike on modern Earth, mafic crust apparently could survive for more than 1 billion y

107 ghts into how microorganisms in the plutonic crust are able to survive within fractures or porous sub

108 ms required to induce foundering in deep arc crust are assessed using an example of representative lo

109 a transport and dyke propagation through the crust are poorly understood.

110 s entering the upper mantle or lower oceanic crust are trapped in olivine as secondary fluid inclusio

111 Deep-sea hydrogenetic ferromanganese crusts are both potential polymetallic resources and rec

112 cates-the largest constituent of the earth's crust-are excluded owing to their weak second harmonic g

113 olvable (41)K/(39)K effects arise in oceanic crust as a result of hydrothermal alteration.

114 ides: the elastic deformation of the Earth's crust as a result of tidal forces.

115 In California, water storage deforms the crust as snow and water accumulates during the wet winte

116 nd/or modifying large volumes of continental crust, as observed in the continents today.

117 at 240 Ma and culminated with 60-70-km-thick crust at 215 Ma.

118 agnitude of ambient tectonic stresses in the crust at depth.

119 long the melting curve of carbonated oceanic crust at depths of approximately 300 to 700 kilometres,

120 he velocity and density of subducted oceanic crust at lower-mantle conditions remain unknown.

121 m (U) is a ubiquitous element in the Earth's crust at ~2 ppm.

122 nce for rapid melt accumulation in the upper crust before many volcanic eruptions.

123 The indication that the lower crust beneath the LMS was folded and pushed upwards and

124 face of arid soils, building biological soil crust (biocrusts) that provide a variety of ecosystem be

125 Biological soil crusts (biocrusts) soil surface communities of lichens,

126 within three microhabitats: biological soil crusts (biocrusts), soil below biocrusts, and the plant

127 mportant component of desert biological soil crusts (BSCs) and is emerging as a model system for stud

128 on-uniformity in the lava gas content and/or crust bulk density across the patera.

129 odynamical settings for the formation of the crust but only if combined with additional SiO(2) inform

130 rocky planets are mostly covered by basaltic crust, but Earth is unique in that it also has extensive

131 ening mechanisms are active in the upper-mid crust, but healing is not always well-explained.

132 ng the geographic arrangement of continental crust, but the data required to fully test the hypothesi

133 osta Rican forearc is sequestered within the crust by calcite deposition.

134 sidence time in basaltic systems of the deep crust by studying ultramafic nodules from the Borgarhrau

135 ckening by 43%-100% (P < 0.01) and leukocyte crusting by 57% (P < 0.05), and it inhibited ex vivo che

136 hich carbon in sediments and altered oceanic crust can be subducted and the relative contributions of

137 pread hydrothermal alteration of the shallow crust caused by the intrusion of dikes and sills of the

138 baking temperature and time, the higher the crust color change, the lower the oxalate concentration,

139 oved dough handling, bread crumb texture and crust color.

140 ed out in addition to the measurement of the crust colour.

141 functional roles of dryland biological soil crust communities (biocrusts), which are expected to und

142 ensis was present among carbonate and barite crusts, constituting the first record of frenulates amon

143 licate mantle, which is itself overlain by a crust containing an outermost layer of primitive solar n

144 gests that the presence of subducted oceanic crust could provide good explanations for some lower-man

145 any do this to the extent required of desert crust cyanobacteria.

146 Many areas of the Earth's crust deform by distributed extensional faulting and com

147 These volumes of crust depleted in delta(18)O are sufficient to explain t

148 arthquake of year 2008 occurred in the upper crust, directly at the structural discontinuity between

149 nception applies large stresses as the ocean crust domes in response to magma ascension and is loaded

150 describing the fragmentation of continental crust during supercontinental coalescence-breakup cycles

151 nt in chemical weathering of the continental crust during the early Cambrian, which may be a trigger

152 terogeneous lithospheric lid that includes a crust enriched in radiogenic elements.

153 acterized by sterile pustules, erosions, and crusts, EPD is difficult to treat and heals slowly.

154 This crust evolved from a highly mafic bulk composition befor

155 ructural deformation shows that the Tianshan crust experienced strong shortening during the Cenozoic.

156 the chemical composition of the continental crust exposed to weathering and found that shales of all

157 ropanal, whereas hexanal was promoted in the crust fermented with lower yeast level.

158 es planar normal faults in the elastic upper crust, followed by postseismic viscous relaxation occurr

159 d, reactive fluid flow through the subducted crust, following dehydration of the underlying, serpenti

160 lost to the system and is sequestered in the crust for millions of years.

161 data reveal that this large block of Archean crust formed by reworking of much older (>4.2 billion-ye

162 Exactly how felsic crust forms when basaltic magmas are the dominant produc

163 large volumes of basalt flushing through the crust from depth overprint their chemical signatures.

164 fundamental role in fluxing metals into the crust from metasomatised lithospheric mantle.

165 ns of fungal communities in the deep oceanic crust from ~10 to 780 mbsf by combining metabarcoding an

166 ck magnetic study of four hydrogenetic Fe-Mn crusts from the Pacific Ocean (PO-01), South China Sea (

167 The lithified oceanic crust, lower crust gabbros in particular, has remained largely unexpl

168 We showed that inactivation of crust genes caused increases in spore relative hydrophob

169 Typical intraplate continental crust has hydrostatic fluid pressure and a near-surface

170 elling asthenosphere might have led to lower crust heating, facilitating eastward extrusion of the So

171 ip and distribute deformation in the shallow crust hinders efforts to mitigate hazards where faults i

172 pervasive in fault zones cutting the Earth's crust; however, the effect of fluid viscosity on fault m

173 tions influence the evolution of the Earth's crust in a range of tectonic settings.

174 ient overplating and burial of early Martian crust in a stagnant-lid tectonic regime, in which the li

175 d the anomalously low density of the Martian crust in comparison with expectations.

176 de evidence that magma intruded into the mid-crust in early 2017, and again in August of that year, p

177 sed using an example of representative lower crust in SW New Zealand.

178 megameter-scale portion of thickened oceanic crust in the uppermost lower mantle west of the Sea of O

179 Bacterial biomass in the nutrient-rich crust increased three-fold one week after watering, wher

180 ogel, while CV deposition created a discrete crust, indicating that CV electrodes were limited by dif

181 The mineralized weathering crusts inherited REE signature of the granites, but show

182 recycled increasing volumes of cold oceanic crust into the mantle.

183 tectonic plate, with only the warmer, lower crust involved in mantle convection.

184 formation and evolution of the primary lunar crust is based on geochemical systematics from the lunar

185 ntis Bank, Indian Ocean, where Earth's lower crust is exposed at the seafloor.

186 tivity while the volume of melt entering the crust is high, raising the possibility of transitions to

187 The lithified lower oceanic crust is one of Earth's last biological frontiers as it

188 t the field strength within the star's outer crust is orders of magnitude larger than the dipole comp

189 that ~40% to ~65% of the CO(2) in subducting crust is released via metamorphic decarbonation reaction

190 One region of ancient crust is the Hudson Bay terrane of northeastern Canada,

191 synrift sedimentary fill is thickest and the crust is thinnest, suggesting that lithospheric thinning

192 on of planets, brown dwarfs and neutron star crusts is determined by the properties of dense and comp

193 Silicon, the second abundant element in the crust, is beneficial for plant growth, mechanical streng

194 arth's mantle is either stored below the arc crust, is efficiently consumed by microbial activity bef

195 second most abundant nonmetal of the earth's crust, is extremely scarce and mechanistically not well

196 second most abundant element in the earth's crust, is nontoxic, and is a robust material offering hi

197 in the geographic arrangement of continental crust, it is difficult to identify a specific causal mec

198 ission measurements of the desiccated desert crust Leptolyngbya ohadii strain identified (i) reduced

199 cap and stalk), but the group also contains crust-like resupinate fungi, polypores, coral fungi, and

200 r mantle imposed by deformation of the lower crust localizes uplift, which is predicted to take place

201 The lithified oceanic crust, lower crust gabbros in particular, has remained l

202 m is the most abundant (7-8%) in the Earth's crust, making the development of aluminum based catalyst

203 that it also has extensive regions of felsic crust, manifested in the form of continents.

204 The Earth's crust-mantle boundary, the Mohorovicic discontinuity, ha

205 xes in the crust and mantle indicate coupled crust-mantle evolution for more than 2 billion years wit

206 tly a topic of debate, dry lower continental crust may be strong under high-grade conditions.

207 differing the most for heptanal 'fatty cake crust', methional 'potato damp', and 2,5-dimethylpyrazin

208 h the steady state rate at which the Earth's crust moves.

209 hese relationships suggest that the deep arc crust must have primarily involved significant igneous a

210 peridotite exhumed in tectonized slow-spread crust near fracture zones may increase water transport t

211 ds, indicate that carbonated igneous oceanic crust, not sediment, is the primary carbon-bearing reser

212 potato damp', and 2,5-dimethylpyrazine 'cake crust, nutty'.

213 jections of anti-mLAMalpha3 IgG erosions and crusts occurred predominantly around the snout, eyes, an

214 rater transition diameters indicate that the crust of Ceres is neither purely icy nor rocky.

215 We observe strong seismic anisotropy in the crust of southern African cratons by Receiver Function a

216 rallel to the Moho are observed in the lower crust of the basins south of Qilian, which we interpret

217 ilicic plutonic material is generated in the crust of the central South American Cordillera.

218 EE) are dominantly mined from the weathering crusts of granites in South China.

219 y quantifying the composition of continental crust on Hadean and Archean Earth is critical to our und

220 tween 800 and 400 Ma, which oxidized oceanic crust on the seafloor.

221 ential (26)Mg incorporation into the oceanic crust, on average by epsilon(solid-fluid) ~ 1.6 per mill

222 pentine-that is, hydrated mantle rather than crust or sediments-is a dominant supplier of subducted w

223 nts of low-temperature exchange with oceanic crust or that the weathering flux of continentally deriv

224 relaxation occurring within the basal lower crust or upper mantle.

225 on days 10-11 after treatment, without pain, crusting, or ulceration.

226 of much older (>4.2 billion-year-old) mafic crust over a 1.5-billion-year interval of early Earth hi

227 s the growth of a relatively mafic planetary crust over the first 1 to 2 billion years of Earth histo

228 In recent decades, peyssonnelid algal crusts (PAC) have become spatial dominants across large

229 epositional points along the mantle-to-upper crust pathway of magmas and hydrothermal fluids, synthes

230 the beneficial genera Bifidobacterium (bread crust, pilsner and black beers, chocolate and sweet wine

231 The lower crust plays a critical role in the processing of mantle

232 ent by potassium chloride in pizza dough and crusts prepared by a traditional long fermentation proce

233 onents in the evolution of upper continental crust, presenting critical information for large-scale b

234 e elements and thus resemble the continental crust produced in modern subduction settings.

235 This occurs when saltation events break salt crusts produced by the efflorescence of brine in the sal

236 otZ is required for the localization of most crust proteins, while CgeA is at the bottom of the genet

237 dependencies for subcellular localization of crust proteins.

238 predictions of geoneutrino emission from the crust provide the critical test needed to define the man

239 to variations in the flux of basalt into the crust, rather than variations in their crustal storage h

240 of these clays was formed when Mars' primary crust reacted with a dense steam or supercritical atmosp

241 It is thought that the Martian basaltic crust reacted with liquid water during this time to form

242 an be used as an effective tracer of oceanic crust recycled into the mantle, as a diagnostic criterio

243 tions-useful for tracing subducted, recycled crust-relate to high (3)He/(4)He and anomalous (182)W.

244 gests the volume of plutonic material in the crust related to Cordilleran magmatic systems is much la

245 An implicit assumption is that the crust relaxes accumulated stress after each episode.

246 We propose that this thick crust represents a major part of the oceanic plateau tha

247 on and tectonic dismemberment of the oceanic crust, resulting in an irregular seafloor morphology mad

248 ng element/Th ratio of the Upper Continental Crust) reveal maximum values 10 to 40 cm below the surfa

249 agnetic measurements revealed that the Fe-Mn crust samples from the Pacific Ocean and Indian Ocean we

250 The degree of gelatinization in crust samples was significantly reduced with a depletion

251 tic synthesis of hydrocarbons during oceanic crust-seawater interactions.

252 mantle-derived magmas emplaced in the lower crust share a common metallogenic signature with upper c

253 ither primitive nor evolved hydrated Martian crust show noticeably different bulk densities compared

254 We find that the subducted oceanic crust shows a large negative shear velocity anomaly at t

255 the spore polysaccharide layer, and impaired crust structure and attachment to the rest of the coat.

256 tle at convergent margins, where the oceanic crust subducts beneath the continental crust.

257 nce for the presence of a felsic continental crust, such as the elevated (49)Ti/(47)Ti ratios in Arch

258 , the widespread serpentinization of Martian crust suggests that metamorphic hydration reactions play

259 m the chemical weathering of the continental crust supplies a steady supply of essential nutrients ne

260 the biogeochemical cycles of Earth's shallow crust, supporting life, stimulating substrate transforma

261 In contrast, a stronger Asian crust suppresses the plateau formation, while the orogen

262 HAs formation was lower in the crust than previously measured in meat slices subjected

263 Most exposed continental crust that can be dated back to the Archaean eon (4 bill

264 a marked enrichment of copper in the Earth's crust that coincided with the biological use of oxygen,

265 ulting in the formation of a viscous surface crust that hinders diffusion of BaP from the film interi

266 t (more than 3.5 billion years old) basaltic crust that is predicted to have existed if Archaean mant

267 icrobial H(2) consumption within young ocean crust that is tractable and can be iteratively improved

268 ate is a relevant constituent of the Earth's crust that is transferred into the deep Earth through th

269 into the Gulf of Oman, and the nature of the crust that underlies it are, however, unknown.

270 typical mantle but resembles that of oceanic crust that was initially altered by seawater and then de

271 itnessed the production of early continental crust, the emergence of life, and fundamental changes to

272 aced as a succession of sills into the lower crust they generate deep crustal hot zones.

273 e upper crust and exhumation of middle/lower crust through detachment faulting.

274 morphic (P, T) conditions in the continental crust through time might therefore reflect the secular e

275 et as the top of a mechanically strong lower crust thrusting several tens of kilometers underneath Qi

276 force significant quantities of magma in the crust to build laccoliths.

277 metasomatized the thickened eclogitic lower crust to produce high levels of HREE and Mo.

278 Deformation is mechanically coupled from the crust to the asthenosphere, with mantle flow overlaid by

279 ical transport of sulfides across the mantle-crust transition.

280 Yet, little is known about the crust-uppermost mantle structure beneath the basin and i

281 The 3D crust-uppermost mantle structure supports a present-day

282 a from thickened mid-Proterozoic continental crust via two-sided subduction can account for both the

283 the starch digestibility of bread crumb and crust was investigated.

284 This can only be explained if the emerged crust was predominantly felsic (silica-rich) since 3.5 b

285 was folded and pushed upwards and the upper crust was removed by exhumation, supports the concept of

286 iated with more intense toasted odour of the crust, was found in breads with higher NaCl content.

287 responses were observed, especially in soil crusts where Betaproteobacteria, Sphingobacteria, and Ba

288 er phases theorized to exist in neutron star crusts, where the right- and left-handed helical element

289 hment effects are favored in arcs with thick crust, which explains why magmatism and differentiation

290 m the mantle to the lower-to-mid continental crust, which leaves little footprint behind by the time

291 ts, in contrast to hydrous mafic terrestrial crust, which transforms to denser eclogite upon dehydrat

292 However, microbiota in the crust, which was relatively enriched in nutrients and or

293 Chestnut flour darkened crumb and crust while no effects on colour were observed for sourd

294 hase transition in silica, subducted oceanic crust will be visible as high-velocity heterogeneities a

295 , our results suggest that subducted oceanic crust will be visible as low-seismic-velocity anomalies

296 melt generation and segregation in the lower crust with new evidence for rapid melt accumulation in t

297 systems play a crucial role in enriching the crust with volatiles and elements that reside primarily

298 ory features were dominated by a thick brown crust, with marked toasted odor, coupled to yellow and c

299 ks, so the addition of seawater K to oceanic crust would be expected to generate (41)K/(39)K variatio

300 s on the timing of weathering of the Martian crust would help understand its evolution, the availabil