ライフサイエンスコーパス: volcanic

1 hydrous silicate magmas relative to dry rift volcanics.

2 provide a diagnostic indicator of incipient volcanic activity and can serve as an analog for studyin

3 ommunities to perceive emergency warnings of volcanic activity as false alarms.

4 rift experienced a major pulse of explosive volcanic activity between 320 and 170 ka.

5 eastern Australia that displays a record of volcanic activity between 33 and 9 million years ago, wh

6 s, but the potentially devastating impact of volcanic activity has not been considered.

7 r analysis reveals a consistent influence of volcanic activity on regional Central American climate o

8 It also extends the volcanic activity on the UPB by approximately 1 million

9 matic systems represent the vast majority of volcanic activity that poses a threat to human life.

10 cano experienced several episodes of intense volcanic activity, culminated in the effusive flank erup

11 mes is tested against the impact of Vesuvius volcanic activity, in particular the great eruption of A

12 stinguishing it from other forcings, such as volcanic activity, remains a major challenge for palaeoc

13 chamber of a volcano, thus accelerating the volcanic activity.

14 Here we study volcanic aerosol changes in the stratosphere using lidar

15 The residence time of volcanic aerosol from strong eruptions is roughly 2-3 y.

16 inconsistencies in the timing of atmospheric volcanic aerosol loading determined from ice cores and s

17 Volcanic aerosol-induced asymmetrical hemispheric coolin

18 ently, the radiative forcing associated with volcanic aerosols in the lowermost stratosphere (LMS) ha

19 Stratospheric volcanic aerosols reflect sunlight, which reduces evapor

20 use gases, and other natural factors such as volcanic aerosols, have influenced global ocean heat con

21 , forming a basis to constrain fluid flow in volcanic and geothermal systems.

22 Evaluation of volcanic and hydrothermal fluxes to the surface environm

23 d-Cretaceous extinction at this site to both volcanic and meteorite events via climate change.

24 rison of its primary igneous building blocks-volcanic and plutonic rocks-and the processes by which t

25 alysis of a comprehensive global data set of volcanic and plutonic whole-rock geochemistry shows that

26 ulti-decadal summer cooling likely driven by volcanic and/or solar forcing, and associated regional s

27 ination of external forcing, i.e., solar and volcanic, and internal feedbacks, that drives the synchr

28 We present paleomagnetic analyses of volcanic angrites demonstrating that they formed in a ne

29 distinct volcanic sites within the Hellenic Volcanic Arc (HVA).

30 Variations in continental volcanic arc emissions have the potential to control atm

31 Here we use enrichment of boron (B/Zr) in volcanic arc lavas as a proxy to evaluate relative along

32 kinematics of the boundary of the Guanacaste Volcanic Arc Sliver that are timely and essential to any

33 anacaste volcanic arc, herein the Guanacaste Volcanic Arc Sliver.

34 hat the slab's mantle dehydrates beneath the volcanic arc, and may be the main source of fluids trigg

35 t the sliver includes most of the Guanacaste volcanic arc, herein the Guanacaste Volcanic Arc Sliver.

36 The Azores, a mid-Atlantic volcanic archipelago located >1000 km off the European c

37 Remote volcanic archipelagoes represent ideal natural laborator

38 data set for carbon and helium isotopes from volcanic arcs and demonstrated that the carbon isotope c

39 inerals suggest enhanced erosion of Rodinian volcanic arcs and orogens.

40 For some volcanic arcs, the geochemistry of volcanic rocks erupti

41 locally enhances fluid introduction beneath volcanic arcs.

42 e Northern Hemisphere, sub-visible layers of volcanic ash (cryptotephra) are valuable time markers du

43 Key reactants include volcanic ash (source of reactive aluminium) and reactive

44 stick together, accelerating the fallout of volcanic ash and climate-forcing aerosols.

45 track dates on stratigraphically bracketing volcanic ash and pyroclastic density current deposits, i

46 tion, which affects the temperature at which volcanic ash becomes liquid, can vary widely amongst vol

47 U-Pb zircon dates for five volcanic ash beds from the Global Stratotype Section and

48 The ingestion of volcanic ash by jet engines is widely recognized as a po

49 the low number of LIVS typically observed in volcanic ash despite the frequent occurrence of lightnin

50 es that the Amazon basin has been subject to volcanic ash fallout during the recent past; 2) highligh

51 artificial ash cloud created by dispersal of volcanic ash from a second aircraft.

52 ice (AVOID) to examine its ability to detect volcanic ash from commercial jet aircraft at distances o

53 Volcanic ash from explosive eruptions can provide iron (

54 Textural analysis of volcanic ash from Santiaguito volcano in Guatemala revea

55 the first time, airborne remote detection of volcanic ash has been successfully demonstrated from a l

56 describe the first cryptotephra (non-visible volcanic ash horizon) to be identified in the Amazon bas

57 ability of the device to detect and quantify volcanic ash in an artificial ash cloud created by dispe

58 port the first identification of New Zealand volcanic ash in Antarctic ice.

59 used to assess the deposition probability of volcanic ash in jet engines.

60 nterest in finding ways to identify airborne volcanic ash in order to keep airspace open and avoid ai

61 volcanic lightning discharge, when airborne volcanic ash is transformed into lightning-induced volca

62 The use of volcanic ash layers for dating and correlation (tephroch

63 Airborne volcanic ash particles are a known hazard to aviation.

64 quate for the prediction of the behaviour of volcanic ash, leading to overestimates of sticking tempe

65 The sensitivity of past ice sheets to volcanic ashfall highlights the need for an accurate cou

66 clotron resonance (FTICR) mass analysis of a volcanic asphalt sample by acquiring data for 20 Da wide

67 wing on c. 20-cm-deep soils over impermeable volcanic bedrock.

68 ow subsea pools located within the Santorini volcanic caldera of the Southern Aegean Sea, Greece, tha

69 ed to the hostile soil conditions within the volcanic caldera possesses the lowest within-population

70 The interior of this volcanic, caldera-like feature is composed of a warm, da

71 crustal limestone is an important source of volcanic carbon.

72 Toba Caldera, Indonesia, caused the greatest volcanic catastrophe of the last 100 kyr, climactically

73 enetic enclaves they host from the Soufriere Volcanic Center (SVC), a long-lived volcanic complex in

74 onsistent with previously reported values in volcanic centers (delta(15)N = -3.0 to 1.9 per thousand)

75 However, some arc volcanic centers have been active for tens of thousands

76 During this period, at least four distinct volcanic centres underwent large-volume (>10 km(3)) cald

77 g a new DIAL laser remote sensing system for volcanic CO2 (CO2DIAL).

78 tow-yos were used to calculate the amount of volcanic CO2 added to the water column for each surveyed

79 Volcanic CO2 emissions play a key role in the geological

80 ts of oceanic currents produced an estimated volcanic CO2 flux = 6.0 10(5) +/- 1.1 10(5 )kg d(-1) whi

81 1.1 10(5 )kg d(-1) which is ~0.1% of global volcanic CO2 flux.

82 e geological carbon cycle, and monitoring of volcanic CO2 fluxes helps to forecast eruptions.

83 excellent opportunity to study the effect of volcanic CO2 on the seawater carbonate system, the globa

84 We studied an Echinometra species on natural volcanic CO2 vents in Papua New Guinea, where they are C

85 Using volcanic CO2 vents, we tested the indirect effects of oc

86 e 2011 eruption of the Puyehue-Cordon Caulle volcanic complex in Patagonia to explore the genetic imp

87 oufriere Volcanic Center (SVC), a long-lived volcanic complex in the Lesser Antilles arc, were integr

88 The Tharsis region is the largest volcanic complex on Mars and in the Solar System.

89 h resulted in the slow pressurization of the volcanic conduit leading to the hydro-volcanic event in

90 The same lavas, deformed experimentally at volcanic conduit temperature and load conditions, exhibi

91 forming primary pyroclasts upon transport in volcanic conduits and plumes.

92 gmentation processes operating in subsurface volcanic conduits.

93 o detect natural external influences such as volcanic cooling events in the upper-ocean because the r

94 which are only comparable to those found in volcanic crater lakes.

95 nditions, which are of utmost importance for volcanic crisis management.

96 cant implications for the interpretations of volcanic deformation worldwide.

97 eractions between glacial sea level changes, volcanic degassing and atmospheric CO2, which may have m

98 x of sulfur dioxide (SO2) emitted by passive volcanic degassing is a key parameter that constrains th

99 Volcanic degassing is a source of these elements to Eart

100 te its significance, an inventory of passive volcanic degassing is very difficult to produce, due lar

101 phy, but also atmosphere composition through volcanic degassing of CO2 at subduction zones and midoce

102 a corresponding increase in CO2 inputs from volcanic degassing.

103 ence of concentrically layered aggregates in volcanic deposits.

104 dataset, the largest to date from submarine volcanic ecosystems, constitutes a significant resource

105 A detailed survey of the volcanic edifice was carried out using seven CTD-pH-ORP

106 Volcanic edifices are abundant on rocky bodies of the in

107 des new independent evidence of long-lasting volcanic effects on climate and elucidates key aspects o

108 This relationship may improve estimates of volcanic emissions and characterization of eruption size

109 These barites are interpreted as primary volcanic emissions formed by SO2 photochemical processes

110 The largest volcanic emitters outgas carbon with higher delta(13)C a

111 It was a hydro-volcanic eruption and new magmatic material was not dete

112 Tephra deposits result from explosive volcanic eruption and serve as indirect probes into frag

113 nts follow in the two springs after the 1991 volcanic eruption of Mt.Pinatubo.

114 erved compared with that during the inactive volcanic eruption period (1936-1962).

115 During the active volcanic eruption periods (1901-1935 and 1963-1993), sig

116 We found that during active volcanic eruption periods, which correspond to a negativ

117 th's mantle affects the dynamics of melting, volcanic eruption style and the evolution of Earth's atm

118 f this finding is that barring another major volcanic eruption, a detectable acceleration is likely t

119 ciated with the recovery from the El Chichon volcanic eruption.

120 ity across two distinct phenomena: explosive volcanic eruptions (P<0.01) and the recent epoch of glob

121 omparison with approaches to criticality for volcanic eruptions and creep failure.

122 orecast failure scenarios both in the field (volcanic eruptions and landslides) and in the laboratory

123 atmospheric gravity oscillations induced by volcanic eruptions and recorded by pressure sensors can

124 Understanding interactions between volcanic eruptions and the cryosphere (a.k.a. glaciovolc

125 Magmatic intrusions and volcanic eruptions are intimately related phenomena.

126 In addition, the NH volcanic eruptions are more efficient in reducing the NH

127 Terrestrial volcanic eruptions are the consequence of magmas ascendi

128 Limitations in using major volcanic eruptions as a constraint on cloud feedbacks ar

129 Our revised timescale more firmly implicates volcanic eruptions as catalysts in the major sixth-centu

130 heric aerosols from large tropical explosive volcanic eruptions backscatter shortwave radiation and r

131 It is difficult to predict hydro-volcanic eruptions because they are local phenomena that

132 Large volcanic eruptions can have major impacts on global clim

133 Volcanic eruptions can impact the mass balance of ice sh

134 Volcanic eruptions contribute to climate variability, bu

135 This suggests that future volcanic eruptions could substantially affect global wat

136 whose onset coincides with clusters of large volcanic eruptions during the nineteenth and twentieth c

137 , approximately 192-y series of halogen-rich volcanic eruptions exactly at the start of accelerated d

138 Volcanic eruptions have episodically interfered with hea

139 ale, we showed that over the last 110 years, volcanic eruptions have influenced ASM variations on an

140 he world which cover between two and 6 major volcanic eruptions in the 20(th) and late 19(th) century

141 Netherlands and then by using the number of volcanic eruptions in the world.

142 Observations following major volcanic eruptions indicate that aerosol enhancements co

143 if unavoidable natural events such as major volcanic eruptions interact with anthropogenic warming u

144 been proposed that a decreasing pressure of volcanic eruptions led to the oxygenation of the atmosph

145 magnitude to Pinatubo and Agung, the largest volcanic eruptions of the 20th century.

146 ycles were excited following five Agung-like volcanic eruptions of the last millennium.

147 Ptolemaic vulnerability to volcanic eruptions offers a caution for all monsoon-depe

148 Large volcanic eruptions on Earth commonly occur with a collap

149 ice cores and can be strongly influenced by volcanic eruptions or anthropogenic emissions.

150 an 3sigma variability coinciding with either volcanic eruptions or possible wild fire activity.

151 Silicic volcanic eruptions pose considerable hazards, yet the pr

152 Following large explosive volcanic eruptions precipitation decreases over much of

153 in order to remove the residual signal from volcanic eruptions present in the OMI data.

154 Large volcanic eruptions produce sulfur dioxide, which in turn

155 Volcanic eruptions provide tests of human and natural sy

156 Volcanic eruptions transfer huge amounts of gas to the a

157 After volcanic eruptions triggered population displacements in

158 Silicic calderas form during explosive volcanic eruptions when magma withdrawal triggers collap

159 Ground deformation often precedes volcanic eruptions, and results from complex interaction

160 hydrocarbon reserves, magma build-up before volcanic eruptions, and subterranean tunnels.

161 sponse.El Nino tends to follow 2 years after volcanic eruptions, but the physical mechanism behind th

162 mplex systems such as the Earth's climate to volcanic eruptions, extreme events or geoengineering.

163 t of aeolian dust and of ash from occasional volcanic eruptions, indicating that metallurgic producti

164 fore material failure and broadly applied to volcanic eruptions, landslides and other phenomena.

165 accumulation in the upper crust before many volcanic eruptions.

166 , reduced solar activity and strong tropical volcanic eruptions.

167 magma chamber dynamics and the triggers for volcanic eruptions.

168 ttrition is likely to occur in all explosive volcanic eruptions.

169 arried out in the aftermath of invasions and volcanic eruptions.

170 ds subsurface reservoirs that are drained by volcanic eruptions.

171 ), which has impacts analogous to those from volcanic eruptions.

172 spheric SO2 emitted from biomass burning and volcanic eruptions.

173 gth and the effusive-explosive transition in volcanic eruptions.

174 w-density pumice clasts generated by silicic volcanic eruptions.

175 deposition of ash sourced from high-latitude volcanic eruptions.

176 of the volcanic conduit leading to the hydro-volcanic event in September 2014.

177 uption (Southern Italy) is the largest known volcanic event in the Mediterranean area.

178 ed on the response of SASM to 34 significant volcanic events using the superposed epoch analysis, the

179 n, intensifying fronts, and even seismic and volcanic events.

180 Volcanic explosions release large amounts of hot gas and

181 is influenced by tectonic, petrological and volcanic factors.

182 ne of the largest active continental silicic volcanic fields in the world.

183 cooling was proportional to the magnitude of volcanic forcing and persisted for up to ten years after

184 y variability and demonstrate that solar and volcanic forcing coupled with ocean circulation dynamics

185 , using climate model output, ice-core-based volcanic forcing data, Nilometer measurements, and ancie

186 nts using the superposed epoch analysis, the volcanic forcing may drive a weak SASM in the second yea

187 here is enhanced significantly by the remote volcanic forcing occurring in the other hemisphere.

188 Here, we focus on strong volcanic forcing since large eruptions are known to be a

189 causal relationship between solar activity, volcanic forcing, and climate as reflected in well-estab

190 This remote volcanic forcing-induced intensification is mainly throu

191 tions that occurred primarily in response to volcanic forcing.

192 the response of the atmosphere to solar and volcanic forcing.

193 ennium quantification of climate response to volcanic forcing.

194 kes an important contribution to the overall volcanic forcing.

195 upper-ocean because the radiative effect of volcanic forcings is short-lived.

196 c thickness is less than 110 kilometres; (2) volcanic gaps in regions where lithospheric thickness ex

197 , permitted a massive release of nickel-rich volcanic gas and subsequent global dispersal of nickel r

198 he carbon isotope composition of mean global volcanic gas is considerably heavier, at -3.8 to -4.6 pe

199 arameter that constrains the fluxes of other volcanic gases (including carbon dioxide, CO2) and toxic

200 Dome reservoir due to the emplacement of hot volcanic gases 1.2-1.5 Ma.

201 The S/(3)He ratios of high-temperature volcanic gases show sulphur flux of 720 Gmol/y at arc vo

202 Microbial corrosion textures in volcanic glass from Cenozoic seafloor basalts and the co

203 glasses, or the biogeochemical weathering of volcanic glasses in seawater.

204 the stratigraphic record and is evidence of volcanic halogen degassing and its potential role for th

205 nd ecosystems should systematically consider volcanic halogen emissions in addition to sulfur emissio

206 Our findings emphasise the significance of volcanic halogens for stratosphere chemistry and suggest

207 ng dynamic models of the magmatic system for volcanic hazard assessment.

208 minin ancestors; and also for evaluating the volcanic hazards posed to the 10 million people currentl

209 that pose unique and previously unrecognized volcanic hazards.

210 lood basalt unit, strengthening the case for volcanic Hg as the driver of sedimentary Hg/TOC spikes.

211 s is substantially hindered by an incomplete volcanic history and an underestimation of the potential

212 igocene basins at a similar latitude and the volcanic history of the Lhasa terrane, we infer that lar

213 1), which infects Sulfolobus solfataricus in volcanic hot springs at 80 degrees C and pH 3.

214 Volcanic hotspot lavas, like those erupted at Hawaii and

215 Volcanic hotspot tracks featuring linear progressions in

216 e silica (amorphous SiO2.nH2O) in an ancient volcanic hydrothermal setting in Gusev crater.

217 ons are compatible with an origin of life in volcanic-hydrothermal sub-seafloor flow ducts.

218 nd suggest that modelling of past and future volcanic impacts on Earth's ozone, climate and ecosystem

219 Perm Anomaly could be linked to the Emeishan volcanics, in contrast to the previously proposed Siberi

220 ing a range of meteorological conditions and volcanic influence.

221 ntribution of carbon release associated with volcanic intrusions in the North Atlantic Igneous Provin

222 Isla Mocha, a volcanic island 35 km offshore of Central-South Chile, i

223 Volcanic island inception applies large stresses as the

224 ere is currently limited information on when volcanic islands are initiated on the seafloor, and no i

225 rical activity in sediments from freshwaters volcanic lakes.

226 les that would occur on the early Earth when volcanic land masses emerged from the ocean over 4 billi

227 mn stability, tephra dispersal, aggregation, volcanic lightening generation, and has concomitant effe

228 A similar process occurs as the result of volcanic lightning discharge, when airborne volcanic ash

229 pact source representing the rate of erupted volcanic mass.

230 ed by impact-ejected material and by erupted volcanic material, but that it survives as a mostly cohe

231 perties is key to enhancing our knowledge of volcanic mechanisms and corresponding risk.

232 The most viscous volcanic melts and the largest explosive eruptions on ou

233 Radioisotopic dating of volcanic minerals is a powerful method for establishing

234 and depauperate intervals, consistent with a volcanic origin for the Hg.

235 behavior provides evidence that continental volcanic outgassing drove long-term shifts in atmospheri

236 les of rotation, and a possible link between volcanic outgassing from Tharsis and the stability of li

237 transplant experiments along a shallow water volcanic pCO2 gradient to assess the importance of the t

238 Our findings confirm the occurrence of a volcanic photochemical pathway specific to the early red

239 observed akaganeite was formed in the Deccan volcanic plume and was transported to the Atlantic and T

240 asurements of key chemical components of the volcanic plume from Kilauea on the Island of Hawai'i.

241 te generated by thermal shock from impact or volcanic plume lightning on ancient Mars.

242 bonyl sulfide (OCS) shielding in an evolving volcanic plume.

243 underscores the chemically dynamic nature of volcanic plumes, which may have important implications f

244 rstanding of how the melt structure controls volcanic processes.

245 xico) and the eruption of the massive Deccan volcanic province (India) are two proposed causes of the

246 causal events: eruption of the Deccan Traps volcanic province and impact of the Chicxulub meteorite.

247 ow eruptive compositions of a single martian volcanic province change over time.

248 rate compositional variation within a single volcanic province on Mars.

249 e for the present equatorial position of the volcanic province.

250 tional evolution of Elysium, a major martian volcanic province.

251 ion from the surface boundary layer explains volcanic provinces such as Yellowstone, Hawaii, and Samo

252 g body of independently measured plutonic-to-volcanic ratios suggests the volume of plutonic material

253 Although the plutonic-to-volcanic ratios we estimate vary along the length of the

254 s are consistent with results from other arc volcanic reservoirs and suggest that arc magmas are gene

255 Recently the case has been made that volcanic reservoirs are rarely molten and only capable o

256 history of reef fishes that are endemic to a volcanic ridge of seamounts and islands to understand th

257 undaries, the Krafla segment of the Northern Volcanic Rift Zone in Iceland and the Manda-Hararo segme

258 rge flows of water, heat and solutes through volcanic rock outcrops on ridge flanks.

259 ium (Cupriavidus metallidurans CH34) can use volcanic rock to satisfy some elemental requirements, re

260 or sources; and (v) selective circulation of volcanic rock tools from a single source.

261 For some volcanic arcs, the geochemistry of volcanic rocks erupting above subducted oceanic fracture

262 r silicic magmas are more likely to generate volcanic rocks than plutonic rocks.

263 nd effective pressure on the permeability of volcanic rocks with a wide range of initial porosities (

264 ) of macroalgae along a gradient of CO2 at a volcanic seep, and examined how shifts in species abunda

265 We address this issue using a 1500-year volcanic sensitivity simulation by the Community Earth S

266 We find that the nakhlites sample a layered volcanic sequence with at least four discrete eruptive e

267 te for silicic differentiation at a range of volcanic settings globally, imaging them remains challen

268 we examined microbial mats from two distinct volcanic sites within the Hellenic Volcanic Arc (HVA).

269 We report here the first volcanic SO2 emissions inventory derived from global, co

270 On average over the past decade, the volcanic SO2 sources consistently detected from space ha

271 anic soil, relative to both H. belmoreana on volcanic soil and H. forsteriana on calcareous soil.

272 na is restricted to, but more successful on, volcanic soil, indicating a trade-off in adaptation to t

273 significantly depleted in H. forsteriana on volcanic soil, relative to both H. belmoreana on volcani

274 species combination except H. forsteriana on volcanic soil.

275 forsteriana can grow on both calcareous and volcanic soils, H. belmoreana is restricted to, but more

276 hic acidobacterium isolated from New Zealand volcanic soils, persist by scavenging the picomolar conc

277 at several thousands of kilometers from the volcanic source.

278 ic ash is transformed into lightning-induced volcanic spherules (LIVS).

279 nally-equivalent eruptive events in regional volcanic stratigraphies.

280 (36)S values, which are best interpreted as volcanic sulfate aerosols formed from OCS photolysis.

281 ss, it was due to heterogeneous chemistry on volcanic sulfate aerosols involving chlorine of anthropo

282 Explosive volcanic super-eruptions of several hundred cubic kilome

283 g the compositional range of the Yellowstone volcanic system and find that in a narrow compositional

284 egmented dyke intrusion in the Baretharbunga volcanic system grew laterally for more than 45 kilometr

285 Defining the magma storage conditions of a volcanic system is a major goal in modern volcanology du

286 ation of discrete melt bodies within the sub-volcanic system that continued to independently fraction

287 flank eruptions at Stromboli and at similar volcanic systems (e.g. Etna, Piton de La Fournaise, Kila

288 Many volcanic systems around the world are located beneath, o

289 of pre-eruptive magmatic processes in active volcanic systems is paramount to understand magma chambe

290 ion and eruption dynamics of Earth's largest volcanic systems, resulting in a better understanding of

291 At a larger scale in volcanic terranes, hybrid events are used empirically to

292 chain, but the emergence of two sub-parallel volcanic tracks along this chain, Loa and Kea, and the s

293 oincides with the appearance of other double volcanic tracks on the Pacific plate and a recent azimut

294 were determined for two soils (semiarid and volcanic) under a range of environmentally relevant temp

295 from changes in the tremor source related to volcanic vent erosion.

296 A pH gradient associated with a natural volcanic vent system within Levante Bay, Vulcano Island,

297 rimitive basaltic to felsic compositions for volcanic versus plutonic samples are generally indisting

298 rovince (CAMP), and release of CO2 and other volcanic volatiles has been implicated in the extinction

299 Two sites in the volcanic zone of Campi Flegrei (Italy) were scanned, yie

300 ircon crystals from an eruption of the Taupo Volcanic Zone, New Zealand.