ライフサイエンスコーパス: crustal

1 Strawn gas is significantly more enriched in crustal (4)He*, (21)Ne*, and (40)Ar* than Barnett gas.

2 oncentrations are positively correlated with crustal (4)He, (21)Ne, and (40)Ar and suggest that noble

3 finding suggests that two distinct modes of crustal accretion occur along slow-spreading ridges.

4 ridor along the Vema Fracture Zone, covering crustal ages from 0 to 100 Ma, show rock exposures occur

5 100 Ma, show rock exposures occurring at all crustal ages.

6 the proportion of high- and low-temperature crustal alteration, or a combination of these and other

7 ion is broadly representative of the average crustal and "bulk Earth" (238)U/(235)U composition.

8 ws that Barnett and Strawn gas have distinct crustal and atmospheric noble gas signatures, allowing c

9 Interactions between crustal and mantle reservoirs dominate the surface inven

10 Here we present detailed constraints on crustal and upper mantle structure from wide-angle seism

11 Here we present the crustal and upper mantle structures along two receiver f

12 At lower-crustal and upper-mantle depths, the boundary between th

13 Teragram quantities of crustal and volcanic aerosol are released into the atmos

14 Upwind PM was enriched in crustal and wood combustion sources while downwind PM wa

15 d organic matter during subsurface mixing in crustal aquifers.

16 present the first comprehensive view of the crustal architecture and uplift mechanisms for the Gambu

17 up to 2 orders of magnitude over the normal crustal As abundances.

18 sitions, we propose 'progressively inhibited crustal assimilation' (PICA) as a major cause of bimodal

19 stematics offer insight into some aspects of crustal assimilation.

20 eexisting crust making up the prebatholithic crustal basement, but the accompanying O and Mg isotope

21 er propose that the rate of energy flow from crustal blocks can control the slip velocity during eart

22 ow that in the early Earth, relatively small crustal blocks, analogous to modern microplates, progres

23 port and rotation of large buoyant water-ice crustal blocks, and pitting, the latter likely caused by

24 Interaction between magma and crustal carbonate at active arc volcanoes has recently b

25 Subduction focus the largest recycling of crustal carbonates and the most intense seismic activity

26 exhumation, supports the concept of a lower crustal channel flow beneath Eastern Tibet.

27 It also influences ocean and crustal chemistry, provides a basis for chemosynthetic e

28 This rapid release of large volumes of crustal CO(2) may impact global carbon cycling.

29 monstrate highly efficient remobilisation of crustal CO(2) over geologically short timescales of thou

30 f the samples reflected the dominance of the crustal component of sand from the Sahara desert, althou

31 however, of the return of subducted oceanic crustal components from the lower mantle.

32 K-feldspar-depleted rocks that were abundant crustal components on ancient Earth.

33 imple crystallization models using this bulk crustal composition as the parental melt accurately pred

34 Apart from complications in assessing early crustal composition introduced by crustal preservation a

35 volved from an approximately average martian crustal composition to one influenced by alkaline basalt

36 s tectonics and evidence for a heterogeneous crustal composition; its north pole displays puzzling da

37 neous Province, and the ubiquity of suitable crustal compositions, we propose 'progressively inhibite

38 and the rock uplift that led to it, invoking crustal compression or extension.

39 locations by factors of 100-3000 compared to crustal concentrations.

40 show that folded crystalline rocks in upper crustal conditions exhibit dramatic strength heterogenei

41 ometers) unaffected by degassing and shallow crustal contamination.

42 eaffirm that tin belt magmas contain greater crustal contributions than copper arc rocks.

43 esent a significant mode of off-axis oceanic crustal cooling not previously recognized or accounted f

44 nisotropy would improve our understanding of crustal deformation and flow patterns resulting from tec

45 nificant but unexplored potential impacts on crustal deformation and seismicity.

46 plift are key to understanding the impact of crustal deformation and topographic growth on atmospheri

47 After a large subduction earthquake, crustal deformation continues to occur, with a complex p

48 Great earthquakes cause large coseismic crustal deformation in areas hundreds of kilometres away

49 , partially due to the challenging nature of crustal deformation measurements at offshore plate bound

50 upper mantle leads to prolonged postseismic crustal deformation that may last several decades and ca

51 tly focus on the different styles of Tibetan crustal deformation, yet these do not readily explain th

52 thick, mafic lower crust and consequent deep crustal delamination and melting--leading to abundant to

53 samples collected near the Sahara have near-crustal delta(56)Fe, soluble aerosols from near North Am

54 At crustal depths, our results support an exhumed mantle ba

55 heral subsidence may result from a large mid-crustal diapir fed by partial melt from the Altiplano-Pu

56 This evidence for early crustal differentiation implies that the Martian crust,

57 the role of mafic cumulates as a residue of crustal differentiation.

58 Crustal dismemberment with or without the development of

59 Crustal displacement is largely accounted for by an annu

60 l properties can change in response to large crustal earthquakes.

61 upgraders (vanadium, nickel, and zinc), and crustal elements (aluminum, iron, and lanthanum), which

62 other chemical parameters (e.g., marine and crustal elements, delta(13)C, delta(15)N, organic carbon

63 During this period, the flux and crustal enrichment factors of the toxic trace metals wer

64 ic zircon that suggest a late Neoproterozoic crustal erosion and sediment subduction event of unprece

65 -rich layer with the help of a parameterized crustal evolution model; we find that the primordial cla

66 rucial to understanding the first 500 Myr of crustal evolution of Earth.

67 overriding plate is subjected to episodes of crustal extension and back-arc basin development, often

68 ults in the central Italian Apennines, where crustal extension and devastating earthquakes occur in r

69 volution as it signifies the localization of crustal extension and rift-related volcanism.

70 tonic and volcanic processes associated with crustal extension become confined to narrow magmatic rif

71 sistent with regional stress estimates and a crustal fault network geometry inferred from seismic and

72 In the context of crustal faulting dynamics, these results suggest that ev

73 y of the sliver, although a system of active crustal faults has been described in central Costa Rica.

74 hed by sequential, oceanward-younging, upper crustal faults, and is balanced through lower crustal fl

75 esults indicate a strong correlation between crustal faults, crustal highs and fluid accumulations in

76 l as an increase in geothermal gradient over crustal faults.

77 It also reveals crustal features at depth that aid in the tectonic recon

78 Furthermore, the inferred present-day crustal fields can account for the lack of solar wind io

79 We uncover a phenomenon-crustal fingering-and demonstrate how it may control met

80 in triggering crustal weakening and outward crustal flow in the expansion of the Tibetan Plateau.

81 ted in the lithosphere cause uplift, and (2) crustal flow, in which low-viscosity material in the low

82 rustal faults, and is balanced through lower crustal flow.

83 es, potentially enabling transit through hot crustal fluids.

84 hat ancient pockets of water can survive the crustal fracturing process and remain in the crust for b

85 ermochronology on volcanically exhumed lower crustal fragments.

86 ifornia, such as subduction-captured oceanic crustal fragments.

87 to form an important source rock for Archean crustal genesis.

88 ly terrestrial impacts, and their effects on crustal growth and evolution, are unknown.

89 A marked decrease in the rate of crustal growth at ~3 billion years ago may be linked to

90 Volcanism is a substantial process during crustal growth on planetary bodies and well documented t

91 lion years--a span that includes continental crustal growth, atmospheric evolution, and the initiatio

92 largely independent of the strength of deep crustal heating.

93 s demonstrate the extremes in variability of crustal helium efflux on geologic timescales and imply c

94 s with chemistry and isotopic analyses, that crustal helium-4 emission rates from Yellowstone exceed

95 ns potentially affected by mantle processes, crustal heterogeneity and active tectonics.

96 However, crustal heterogeneity has prevented a thorough geochemic

97 a strong correlation between crustal faults, crustal highs and fluid accumulations in the overlying s

98 ta, we map tectonic features such as faults, crustal highs, and indicators of fluid flow processes.

99 ts of interconnected fluid from the earliest crustal history.

100 ills into the lower crust they generate deep crustal hot zones.

101 as reactions between melt and mush in lower crustal 'hot zones' produce amphibole-rich assemblages,

102 The degree and extent of crustal hydrothermal alteration related to the eruption

103 us and the resulting slow reduction in ocean crustal hydrothermal exchange throughout the early Terti

104 of mantle that has experienced little or no crustal interaction.

105 The limited distribution of lower crustal intrusions implies modest total CAMP volumes of

106 Interaction between water and crustal iron minerals yields H(2) that partition into th

107 bove the quartz alpha-beta phase transition, crustal kappa is nearly independent of temperature, and

108 We image the low P-wave velocity crustal layer on the slab top and show that it disappear

109 n the Moho transition zone (MTZ) and the mid-crustal lens, consistent with geophysical studies that s

110 ns originating from magma accumulated in mid-crustal lenses at the spreading axis, but the style of a

111 agnitude above what is considered background crustal levels.

112 nate platforms, indicating that reworking of crustal limestone is an important source of volcanic car

113 We find that the pH of fluids in subducted crustal lithologies is confined to a mildly alkaline ran

114 s Basin), both elements resulting from supra-crustal loading of the Lhasa block by the Zangbo Complex

115 t formation within the martian mantle due to crustal loading.

116 a thermal gradient, a likely scenario within crustal mafic rocks on the early Earth, drive a complex,

117 This lower-crustal magma body has a volume of 46,000 cubic kilomete

118 smic inversion, we revealed a basaltic lower-crustal magma body that provides a magmatic link between

119 three decades, the classical focus on upper crustal magma chambers has expanded to consider magmatic

120 erived magmas transit the crust and recharge crustal magma chambers.

121 bic kilometers, ~4.5 times that of the upper-crustal magma reservoir, and contains a melt fraction of

122 monly occur with a collapse of the roof of a crustal magma reservoir, forming a caldera.

123 mantle plume and the previously imaged upper-crustal magma reservoir.

124 Our results show clear evidence of mid-crustal magma storage beneath the depths of located volc

125 Here we show direct evidence for mid-crustal magma storage beneath the frequently erupting Cl

126 To better examine the role of crustal magmatic processes and its relationship to erupt

127 Effective mingling within upper crustal magmatic reservoirs obscures a compositional bim

128 rupting volcanoes where well-developed trans-crustal magmatic systems are likely to exist, due to a l

129 Lower crustal magmatism is concentrated where synrift sediment

130 eophysical applications including mapping of crustal magnetism and ocean circulation measurements, ye

131 traints on the length of time that subducted crustal material can survive in the mantle, and on the t

132 th elements in enriched shergottites lies in crustal material incorporated into melts or in mixing be

133 results suggest that subduction of oxidized crustal material may not significantly alter the redox s

134 Factors associated with traffic and crustal material showed consistently positive associatio

135 lumes of older compositionally heterogeneous crustal material to have created the Vestoids and howard

136 e of at least (3.4 +/- 0.2) x 10(6) km(3) of crustal material was removed and redistributed during ba

137 rimarily mechanically generated and includes crustal material, brake and tire wear, and biological pa

138 actors with species associated with traffic, crustal material, residual oil, and coal.

139 to which Martian magmas may have assimilated crustal material, thus altering the geochemical signatur

140 Earth's crust during geological recycling of crustal material.

141 9-11 N degrees introduces overlying forearc crustal materials into the Costa Rican subduction zone,

142 dust episode: simple quantification of bulk crustal materials may have misappropriated this elevated

143 Crustal materials, the major component of CPM, demonstra

144 noes are thought to sample ancient subducted crustal materials.

145 en any K-isotope analyses of altered oceanic crustal materials.

146 from iron/steel manufacturing (36% +/- 9%), crustal matter (33% +/- 11%), and coal combustion (11% +

147 burning, motor vehicles, marine aerosol and crustal matter.

148 ore silicic activity given a decrease in the crustal melt flux.

149 Until now, only seismic reflections from mid-crustal melt lenses and sills within the MTZ have been d

150 action in basalts, and in indicators of deep crustal melting and fractionation, such as Na/K, Eu/Eu*

151 It is inferred that crustal melting played a key role in triggering crustal

152 y high radiogenic heat production to achieve crustal melting temperatures.

153 that fractional crystallization, rather than crustal melting, is predominantly responsible for the pr

154 s geochemical signal is likely to display a 'crustal memory effect' following increases in atmospheri

155 d over the past two million years by intense crustal metamorphism induced by the Yellowstone hotspot.

156 from brake wear (primarily Cu, Pb, Zn), (2) crustal minerals (primarily Al, V, Fe), (3) metals media

157 lattice-preferred orientation of anisotropic crustal minerals caused by extensional deformation.

158 ogenic sources were significantly diluted by crustal minerals coincident with the large-scale Saharan

159 so able to determine that local emissions of crustal minerals dominated the period immediately follow

160 The new crustal model reveals strong heterogeneity, including lo

161 Histories of vertical crustal motions at convergent margins offer fundamental

162 Geodetic investigations of crustal motions in the Amundsen Sea sector of West Antar

163 iers, the water cycle, steric expansion, and crustal movement is challenging, especially on regional

164 describe the long-term surface recycling of crustal NMD anomalies, and show that the record of this

165 The similarity of Strawn and stray gas crustal noble gas signatures suggests that the Strawn is

166 ce of CO(2) and a mantle and/or lower-middle crustal origin for at least part of the degassed carbon.

167 Crustal pathways connecting deep sources of melt and the

168 s deeper off-axis flow is strongly shaped by crustal permeability, particularly the brittle-ductile t

169 trace element geochemistry as a major lower crustal phase, amphibole is neither abundant nor common

170 r(-1) of right lateral motion of the Pacific crustal plate northwestward past the North American plat

171 ., within 1 My, depending on the size of the crustal plug.

172 Thick continental crustal plugs can cause rapid necking while smaller plug

173 e a common metallogenic signature with upper crustal porphyry-epithermal ore systems.

174 Imaging the mid- to lower-crustal portions (here, ~5-15 km and >15 km respectively

175 sing early crustal composition introduced by crustal preservation and sampling biases, effects such a

176 Resolving the timing of crustal processes and meteorite impact events is central

177 trically more extensive with ~ 1060 m of the crustal profile forming between ~ 2.02 and ~ 1.66 Ma, fo

178 at across-strike and along-strike changes in crustal properties at the Eastern Lau spreading centre a

179 Crustal properties of young oceanic lithosphere have bee

180 We infer that the abrupt changes in crustal properties reflect rapid evolution of the mantle

181 accounting for magma buoyancy, viscoelastic crustal properties, and sustained magma channels.

182 logitic lithospheric inclusions derived from crustal protoliths.

183 Here we show that the abundance of crustal quartz, the weakest mineral in continental rocks

184 States reveal strong deep (middle to lower)-crustal radial anisotropy that is confined mainly to the

185 The coincidence of crustal radial anisotropy with the extensional provinces

186 Although observations of crustal radial anisotropy would improve our understandin

187 as 2.4, substantially lower than the typical crustal ratio of 10.

188 the demise of continental ice sheets induced crustal rebound in tectonically stable regions of North

189 hur reservoirs are connected via subduction, crustal recycling and volcanism.

190 ns they cannot reveal temporal variations in crustal recycling over Earth history.

191 t underutilized repository for interrogating crustal recycling through geological time.

192 spheric mantle and/or Ga timescales for deep crustal recycling.

193 vicic discontinuity in thickened continental crustal regions.

194 This field most likely originated from crustal remanence produced by an earlier dynamo, suggest

195 ration of reservoir assembly documents rapid crustal remelting and two to three orders of magnitude h

196 geneities in Earth's deep mantle and shallow crustal reservoirs, as well as Earth's oxidation state.

197 This places firm constraints on the total crustal residence time of mantle-derived magmas and has

198 provides a natural laboratory to explore the crustal response to a quantifiable transient force.

199 both the crust and the mantle, facilitating crustal reworking and planetary differentiation.

200 provide age constraints, is a key archive of crustal reworking.

201 emerging from feedbacks between erosion and crustal rheology active well before 2.5 Ma.

202 numerical models to evaluate the effects of crustal rheology on the formation of the Himalayan-Tibet

203 NWA 7034 is a geochemically enriched crustal rock compositionally similar to basalts and aver

204 this theory, FANs represent the oldest lunar crustal rock type.

205 rom laser-flash analysis for three different crustal rock types, showing that kappa strongly decrease

206 sed as a mechanism for the uplifting of deep crustal rocks ('thick-skinned' deformation) far from pla

207 nic settings, on the mechanical behaviour of crustal rocks are largely unknown.

208 at they were generated by partial melting of crustal rocks at temperatures of 700-1,050 degrees C and

209 Although for crustal rocks both kappa and k decrease above ambient te

210 We also show that the erosion of crustal rocks from whether plumes (mafic in average) or

211 island basalt samples as well as continental crustal rocks going back to 2 Ga are within 1.7 ppm of t

212 Thus Pliocene-Quaternary melting of crustal rocks occurred at depths of 15-50 km in areas wh

213 es (OCCs) that expose upper mantle and lower crustal rocks on the seafloor.

214 nt zinc isotope and abundance data for lunar crustal rocks to constrain the abundance of volatiles du

215 en bulk silicate Earth and lunar basalts and crustal rocks, the volatile loss likely occurred in two

216 ean crust and hydrothermally altered shallow-crustal rocks.

217 tions of seismic structures in exhumed lower crustal rocks.

218 the ferroan anorthosite (FAN) suite of lunar crustal rocks.

219 t a direct tracer for the SiO(2) contents of crustal rocks.

220 ulk mechanical behaviour and permeability of crustal rocks.

221 Opposite to an expected crustal root beneath the orogen, the Moho beneath Qilian

222 ica surrounding the Gamburtsevs, and a thick crustal root beneath the range.

223 s, the mountain range is underlain by a deep crustal root.

224 ate there has been little corroboration from crustal scale geophysical imaging.

225 that the mantle fluids are escaping along a crustal-scale fault marked by clusters of non-volcanic t

226 ult, and subdetachment deformation involving crustal-scale nappe folds and magmatic intrusions, which

227 lium efflux on geologic timescales and imply crustal-scale open-system behaviour of helium in tectoni

228 Both profiles show a crustal-scale outline of the subducting Indian crust.

229 The Kohistan crustal section is negatively buoyant with respect to th

230 ese rocks may represent the oldest preserved crustal section on Earth.

231 Ti isotopes in crustal sediments are still a potential proxy to identif

232 Here we report deep crustal seismic reflections off the southern Juan de Fuc

233 oor dominated by linear abyssal hills, upper crustal seismic velocities abruptly increase by over 20%

234 ems, we present a continuous high-resolution crustal seismic velocity model for an 800 km section of

235 ds rise from 100 km or more and invade upper crustal seismogenic zones that have exhibited historic g

236 between 25 and 10 Ma, a rate consistent with crustal shortening as the dominant driver of surface upl

237 nverged up to 3,600 +/- 35 km, yet the upper crustal shortening documented from the geological record

238 This suggests that crustal shortening is a primary driver for uplift and to

239 ack and transient episodes of orogenesis and crustal shortening, coincident with accretion of exotic

240 alanced geologic cross-sections to show that crustal shortening, structural relief, and topography ar

241 Third, no PGE anomalies distinct from crustal signatures are present in the marine record in e

242 es, while the latter undermines estimates of crustal silica content inferred from terrigenous sedimen

243 that the former complicates efforts to infer crustal silica from compatible or incompatible element a

244 ly explained by a model with nearly constant crustal silica since at least the early Archean.

245 ary reduction in the friction coefficient of crustal silicate rocks results from intense "flash" heat

246 occurring phase in areas containing recycled crustal slabs, which are more oxidized and Ca-enriched t

247 not requiring migration of brines from deep crustal source(s).

248 nt magnetism might suggest an early phase of crustal spreading.

249 o the crust, rather than variations in their crustal storage history.

250 e durations and physical conditions of upper-crustal storage remain highly debated topics in volcanol

251 ta, and a poroelastic model, we computed the crustal strain and pore pressure.

252 Although lower crustal strength is currently a topic of debate, dry low

253 tate friction law, we compute the changes in crustal stress and seismicity rate in Oklahoma.

254 of these conditions to volcanic deformation, crustal stress evolution, and eruption forecasts.

255 The Earth's crustal stress field controls active deformation and ref

256 nd is traditionally used to infer changes in crustal stress over time.

257 oduce observable surface deformation, induce crustal stresses and modulate seismicity rates.

258 The determination of the crustal structure is essential in geophysics, as it give

259 The crustal structure of Orientale provides constraints on t

260 s, dominate the stratigraphy, tectonics, and crustal structure of the Moon.

261 obtained image shows a high-resolution upper crustal structure on a 500 km-long profile that is perpe

262 arside and suggests a relation between lunar crustal structure, nearside volcanism, and heat-producin

263 nomalous (182)W in the geodynamic context of crustal subduction and recycling and informs on survival

264 y 10 metres when we account for post-glacial crustal subsidence of these sites over the course of the

265 ueous fluids is a dynamic process in shallow crustal systems, redistributing nutrients as well as con

266 nditions, approaching 0.5 mm(2) s(-1) at mid-crustal temperatures.

267 ravity anomalies (mass deficits) produced by crustal thickening at the base of the ice shell overwhel

268 In the South Qinling Belt, crustal thickening began at 240 Ma and culminated with 6

269 ember models have been proposed: (1) brittle crustal thickening, in which thrust faults with large am

270 Along with an increase in preserved crustal thickness across the Archaean/Proterozoic bounda

271 However, the farside crustal thickness and the topography it produces may hav

272 geochemistry can be used to track changes of crustal thickness changes in ancient collisional belts.

273 oes and their intrusive equivalents to infer crustal thickness changes over time in ancient orogens.

274 We show that the crustal thickness control of Nb/Ta can be explained by r

275 Then crustal thickness decreased to 45 km at 200 Ma and remai

276 from subduction-related arcs can provide the crustal thickness evolution of an orogen from oceanic su

277 ween whole-rock values of Sr/Y and La/Yb and crustal thickness for intermediate rocks from modern sub

278 ean-ridges basalt chemistry, axial depth and crustal thickness have been ascribed to mantle temperatu

279 sults, we investigate temporal variations of crustal thickness in the Qinling Orogenic Belt in mainla

280 We show that much of the topography and crustal thickness in this terrain can be described by a

281 Our approach predicts a present-day average crustal thickness of 40 +/- 25 kilometres and a surface

282 elt transport predict temporal variations in crustal thickness of hundreds of meters.

283 ghlands and in agreement with the degree-two crustal thickness profile.

284 Our results suggest that crustal thickness remained constant in the North Qinling

285 l parameters can be used to track changes of crustal thickness through time in ancient subduction sys

286 a/Yb is a feasible method for reconstructing crustal thickness through time in continental collisiona

287 of the observed changes in geochemistry and crustal thickness with stepwise atmospheric oxidation at

288 he extent of Nb/Ta fractionation varies with crustal thickness with the lowest Nb/Ta seen in continen

289 From inversion of gravity anomaly data (crustal thickness), analysis of regional magnetic data,

290 thermal gradient at the time of impact, the crustal thickness, and the extent of volcanic fill.

291 whole-rock Sr/Y and La/Yb ratios and modern crustal thickness.

292 Inferred crustal thicknesses using our proposed empirical fits ar

293 and relatively uniform strain in response to crustal thinning and extension.

294 and gravity anomalies and isostasy indicate crustal thinning of more than 1.9 km.

295 creasing seafloor depth, forearc retreat and crustal thinning, for initial Hikurangi Plateau-Kermadec

296 Concentrations of sea salt crustal tracer species, oxalate, and malonate were posit

297 demonstrate a surprising correlation of low crustal v(P)/v(S) with both higher lithospheric temperat

298 t layers investigated are similar to average crustal values, indicating the absence of a significant

299 We use the crustal velocity field of the Plate Boundary Observatory

300 stal melting played a key role in triggering crustal weakening and outward crustal flow in the expans

301 with no influence from mantle convection or crustal weakness necessary.