ライフサイエンスコーパス: volcanic

1 -spreading ridges are a complex interplay of volcanic accretion and tectonic dismemberment of the oce

2 ount in the basin center indicating episodic volcanic activity along the Terceira Rift.

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

4 We discuss the volcanic activity as well as key data streams used to tr

5 This paper provides an overview of the volcanic activity at Mount Agung from the viewpoint of t

6 Synchronicity of (sub)volcanic activity between Taimyr and the Siberian Traps

7 Thus, volcanic activity can be modulated by extreme rainfall t

8 The vast aerial extent of the (sub)volcanic activity during the Siberian Traps main pulse m

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

10 a precision better than ~5 m.y. whether (sub)volcanic activity in these areas actually occurred durin

11 Volcanic activity is often preceded or accompanied by di

12 Volcanic activity occurring in tropical moist atmosphere

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

14 up of blocks created by episodes of intense volcanic activity or tectonic deformation.

15 ce, poorly known-although evidence of recent volcanic activity(1) suggests that its deep interior rem

16 proposed that rainfall can modulate shallow volcanic activity(2,3), but it remains unknown whether i

17 e mercury (Hg), assumed to reflect shifts in volcanic activity, across the Permian-Triassic boundary

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

19 eteorological (hurricanes), and geophysical (volcanic activity, tsunamis).

20 coupling of biotic extinction and increased volcanic activity.

21 , further linking Hg enrichment to increased volcanic activity.

22 Given the unpredictable nature of future volcanic aerosol forcing, it is suggested that a large p

23 ghlights the importance of anthropogenic and volcanic aerosols over GHG in generating forced Sahel ra

24 e forcings-including anthropogenic aerosols, volcanic aerosols, and greenhouse gases (GHG)-relative t

25 and largely linked to the representation of volcanic aerosols.

26 Using volcanic analogues, we consider the structural form of t

27 e possible for Etna and, by extension, other volcanic and anthropogenic sources globally.

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

29 and delta(18)O ratios that overlap with the volcanic and plutonic reference materials (> 800 degrees

30 fects can be used as growth-rate proxies for volcanic and subvolcanic minerals.

31 tensional tectonics of the region, pose both volcanic and tectonic hazards to the city of Rome, locat

32 Analyzing examples from Hawaiian volcanic and West Atlantic hurricane interactions, this

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

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

35 As the Kumamoto setting is representative of volcanic aquifer systems at convergent margins where sei

36 well constrained compared to fluxes from the volcanic arc front.

37 lfur concentration, and delta(34)S values in volcanic arc rocks have been attributed to significant s

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

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

40 ctonic uplift during collision of the Panama volcanic arc with South America.

41 -disciplinary project in the Lesser Antilles volcanic arc(3), we studied boron trace element and isot

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

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

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

45 Decades of study on volcanic arcs have provided insight into the overarching

46 er large-scale frontier geologic problems in volcanic arcs.

47 agmatic orogens, particularly in continental volcanic arcs.

48 It stopped abruptly at the Coso volcanic area and at the Garlock Fault and brought some

49 it was concurrent with 50 m of uplift in the volcanic area; (iii) the time since the last eruption (7

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

51 e spectrometer) analyses of five microscopic volcanic ash (cryptotephra) particles extracted from the

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

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

54 Volcanic ash from a vulcanian explosion and from a pyroc

55 outdoor mesocosms of sterile, freshly fallen volcanic ash from the Sakurajima volcano, Japan.

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

57 Volcanic ash is often neglected in climate simulations b

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

59 Coarse-grained volcanic ash leads to significantly higher complexity, w

60 mate model simulations, and of the impact of volcanic ash on stratospheric chemistry and radiation.

61 Volcanic ash particle properties depend upon their genet

62 urrent impulse experiments were performed on volcanic ash samples to determine the magnetic effects t

63 earliest stages of soil biota development of volcanic ash, and how rapidly it can proceed.

64 ay- to sand-sized mineral abrasives (quartz, volcanic ash, loess, kaolin) on DMT in a controlled feed

65 esource to identify generation mechanisms of volcanic ash, which is pertinent to volcanology, aviatio

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

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

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

69 crustal limestone is an important source of volcanic carbon.

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

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

72 Ash-rich particles dominate the volcanic cloud optical properties for the first 60 days.

73 a global scale, which appear attributable to volcanic CO(2) and mercury emissions.

74 4,900 petagrams of carbon (PgC), pointing to volcanic CO(2) emissions as the main carbon source respo

75 present an updated evaluation of the world's volcanic CO(2) emissions that takes advantage of recent

76 Past attempts to extrapolate the global volcanic CO(2) flux have been biased by observations bei

77 Our results reveal a global volcanic CO(2) flux of 51.3 +/- 5.7 Tg CO(2)/y (11.7 x 1

78 isk assessment and calculation of the global volcanic CO(2) gas flux.

79 Such large volumes of volcanic CO(2) likely contributed to end-Triassic global

80 quantification of the long-term emissions of volcanic CO(2) to the atmosphere.

81 zard posed by relatively small-scale lateral volcanic collapses, which can occur en-masse, without an

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

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

84 resent new laboratory experiments in a model volcanic conduit, which suggest that these differences i

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

86 gmentation processes operating in subsurface volcanic conduits.

87 nal support for a dynamical response linking volcanic cooling to El Nino remains ambiguous, Robock ra

88 atory and other scientists responding to the volcanic crisis.

89 to make decisions during a complex and tense volcanic crisis.

90 sess the contribution of these conditions to volcanic deformation, crustal stress evolution, and erup

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

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

93 Volcanic degassing is a source of these elements to Eart

94 an effect on atmospheric thickness and that volcanic degassing is most efficient for planets between

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

96 Volcanic degassing of planetary interiors has important

97 suggesting a cause-effect relationship where volcanic degassing triggers global climatic changes.

98 oceanic dissolved inorganic carbon caused by volcanic degassing, global warming, and sea-level rise.

99 We combine (40)Ar/(39)Ar geochronology of volcanic deposits and a geomorphologic/stratigraphic/pal

100 umulation of magma within the Monti Sabatini Volcanic District (MSVD), Italy, coupled with the extens

101 i Albani, it should be regarded as a dormant volcanic district, as the time of 70 kyr elapsed since t

102 d products of the Monti Sabatini and Vulsini volcanic districts, along with a compilation of all the

103 racted from two hot springs within an active volcanic ecosystem on the Kamchatka peninsula, Russia.

104 The overall understanding of the volcanic edifice and its dynamics is thus limited by sur

105 r the organisation of magma transport within volcanic edifices, and the evolution and stability of lo

106 Eruptive activity shapes volcanic edifices.

107 alculated to track the temporal variation of volcanic elastic radiation, and the lava fountain height

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

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

110 , many potentially endemic to this submarine volcanic environment.

111 tal significance in the iron and sulfur-rich volcanic environments of early earth and possibly the or

112 obial colonization and community dynamics in volcanic environments.

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

114 Future work is needed to confirm that a volcanic eruption from Mt.

115 has been attributed in previous studies to a volcanic eruption from the submarine Kuwae caldera in Va

116 ians have previously speculated that a large volcanic eruption of unknown origin was the most likely

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

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

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

120 4)He ratio detectors aimed at earthquake and volcanic eruption studies, and monitoring of nuclear sit

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

122 environmental impact of the Thera/Santorini volcanic eruption.

123 We assess the main external forcings (i.e., volcanic eruptions and solar activity) on NAO variabilit

124 Explosive volcanic eruptions are the largest non-anthropogenic per

125 Volcanic eruptions are thought to be a key driver of rap

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

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

128 to the occurrence of several closely spaced volcanic eruptions between 1108 and 1110 CE.

129 essing of mantle melts and the triggering of volcanic eruptions by supply of magma from greater depth

130 Volcanic eruptions can affect global climate through cha

131 Volcanic eruptions can impact the mass balance of ice sh

132 limate response to large volcanic eruptions: Volcanic eruptions cool the surface, thus masking the re

133 Finally, our analysis suggests that volcanic eruptions do not lead to an overall global redu

134 1477) claimed that large volcanic eruptions do not produce a detectable El Nino r

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

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

137 However, identification of stratospheric volcanic eruptions in the geological record and their ca

138 Observations following major volcanic eruptions indicate that aerosol enhancements co

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

140 sults suggest that warming induced by future volcanic eruptions may further enhance the vulnerability

141 illion years ago suggests that stratospheric volcanic eruptions may have contributed to synergetic en

142 pan-tropical surface cooling caused by large volcanic eruptions may mask El Nino warming at our centr

143 em Model to investigate the impact of strong volcanic eruptions occurring in the tropical Northern (N

144 al Pacific to gauge ENSO's response to large volcanic eruptions of the last millennium.

145 six Arctic ice cores that one of the largest volcanic eruptions of the past 2,500 y occurred in early

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

147 The effect of the volcanic eruptions on the ITCZ and hence on TC activity

148 Natural drivers such as large explosive volcanic eruptions or multidecadal cycles in ocean circu

149 Silicic volcanic eruptions pose considerable hazards, yet the pr

150 Large volcanic eruptions produce sulfur dioxide, which in turn

151 Volcanic eruptions provide tests of human and natural sy

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

153 t affect eruptive behavior occur during many volcanic eruptions, but typical analytical techniques ar

154 High quality records of stratospheric volcanic eruptions, required to model past climate varia

155 elta(17)O anomaly of sulfate for the largest volcanic eruptions, showing a further change in atmosphe

156 for investigating the dynamics and timing of volcanic eruptions.

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

158 accumulation in the upper crust before many volcanic eruptions.

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

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

161 ce that are forced by orbital variations and volcanic eruptions.

162 ncies to characterize electrical activity in volcanic eruptions.

163 ceed impacts caused by historic droughts and volcanic eruptions.

164 ed the fundamental climate response to large volcanic eruptions: Volcanic eruptions cool the surface,

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

166 on of Kilauea Volcano was one of the largest volcanic events in Hawai'i in 200 years.

167 a new 2600-year chronology of stratospheric volcanic events using an independent approach that relie

168 Strombolian volcanic explosions are commonly attributed to the rise

169 Here we show using well-dated volcanic fallout records in six Arctic ice cores that on

170 ied beneath lavas of a long-lived, 910-km(3) volcanic field in Southern Laos: 1) Tektite geochemistry

171 ecorded in a newly-recognised Central Panama volcanic field that includes several phases of developme

172 vations that formation of the Central Panama volcanic field was critical in shaping regional topograp

173 The average strike-dimension of volcanic fissures/feeder-dykes in Etna is about 2.7 km.

174 ere we use data on the size distributions of volcanic fissures/feeder-dykes, crater cones, dyke thick

175 egrees C and supported by extensive uneroded volcanic flows.

176 ce, such as bio-foams, froth floatation, and volcanic flows.

177 quitous and dramatic intra-arc variations in volcanic flux and composition remain largely unresolved.

178 ile lower than recent estimates, this global volcanic flux implies that a significant proportion of t

179 -ocean biogeochemistry separated from coeval volcanic fluxes.

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

181 ose models showing a strong ENSO response to volcanic forcing may overestimate the size of the forced

182 Inconclusive results on the volcanic forcing on NAO variability over decadal time-sc

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

184 lumn formed over the volcano and acted as a 'volcanic freezer' containing ~3 x 10(9) kg of ice on ave

185 Volcanics from outside the main Siberian Traps, e.g. Tai

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

187 N(2) as a new tracer of air contamination in volcanic gas effusions.

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

189 s sensing and a new approach to estimate key volcanic gas parameters based on magma compositions.

190 hemistry consistent with mixing of a reduced volcanic gas-influenced end member with an oxidized near

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

192 zones and transform it into fluids, magmas, volcanic gases and diamonds.

193 elationships between the CO(2)/S(T) ratio of volcanic gases and whole-rock trace element compositions

194 that these data imply that reducing Archean volcanic gases could have prevented atmospheric O(2) fro

195 high-precision noble gas isotopic data from volcanic gases emanating from, in and around, the Yellow

196 ce of the largest stratospheric injection of volcanic gases in the Common Era.

197 incorporation of electron donors supplied by volcanic gases) in springs sourced by mixed fluids.

198 n vent volcanoes are major global sources of volcanic gases.

199 t hydrogen isotopic compositions of hydrated volcanic glasses and modern stream waters to determine l

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

201 nsity currents (PDCs) are a life-threatening volcanic hazard.

202 tor that should be considered when assessing volcanic hazards.

203 ing dome growth to improve the assessment of volcanic hazards.

204 on of the arc and its associated seismic and volcanic hazards.

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

206 rived from the continental weathering of the volcanic host rocks.

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

208 vironmental conditions characteristic of the volcanic hot springs in which these archaeal extremophil

209 Volcanic hotspot lavas, like those erupted at Hawaii and

210 res in ocean island basalts (OIB) erupted at volcanic hotspots derive from deep-seated domains preser

211 calcite in calc-silicate xenoliths from arc volcanics in a case study from Merapi volcano (Indonesia

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

213 sent paleomagnetic data from Saint Helena, a volcanic island ideally suited for testing the hypothesi

214 Volcanic island inception applies large stresses as the

215 s related to repeated flank collapses of the volcanic island of Stromboli (Southern Italy) occurred d

216 Ambrym, a basaltic volcanic island, hosts a 12-km wide caldera and several

217 each inside the flooded caldera of an active volcanic island.

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

219 Large-scale landslides at volcanic islands are one of the most dangerous geologica

220 across the Hawaiian archipelago, where these volcanic islands differ in age by several million years.

221 show that analyses of chemically correlated volcanic layers and the palaeomagnetic stratigraphy, com

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

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

224 fects that may result from the occurrence of volcanic lightning during explosive eruptions.

225 dence suggesting that dominantly crystalline volcanic magma reservoirs can be rapidly reactivated by

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

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

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

229 observed in rice paddy fields, landfills, or volcanic mud pots, by preventing the accumulation of inh

230 etion also makes it more difficult for later volcanic outgassing to revive the atmosphere.

231 s to space, magma ocean crystallization, and volcanic outgassing).

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

233 SVD and assess the timing of the most recent volcanic phase.

234 ncrease the potential for rainfall-triggered volcanic phenomena worldwide.

235 M flash energies and lengths observed in the volcanic plume are on the lower end of the flash spectru

236 of bright icy particles or water vapor from volcanic plumes originating on the moon Enceladus.

237 c degassing data available and insights into volcanic processes to the volcanological community.

238 rstanding of how the melt structure controls volcanic processes.

239 n is consistent with the locations of higher volcanic productivity and thicker arc crust.

240 The unequal distribution of volcanic products between the Earth-facing lunar side an

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

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

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

244 ference data from layered intrusions, active volcanic provinces, and established low-temperature and

245 tween these and the main Siberian Traps (sub)volcanic pulse, and the presence of a second Dinerian-Sm

246 ur Hg and Hg/TOC values were associated with volcanic pulses which triggered the massive environmenta

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

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

249 te-volcano connections and improves ice core volcanic reconstructions.

250 nosphere mantle contribution to the Cenozoic volcanic record of the region.

251 cally influenced hydrothermal systems on the volcanic resurgent cones of Brothers volcano harbor comm

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

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

254 Emplacement of large volumes of (sub)volcanic rocks during the main pulse of the Siberian Tra

255 rocks differed markedly from the shales and volcanic rocks of local hills.

256 Here we report new PGE data for volcanic rocks of the Central Atlantic Magmatic Province

257 )He (that is, primordial) signatures in some volcanic rocks suggest that volumes of relatively undiff

258 Kimberlites, small-volume volcanic rocks that are the source of most diamonds, off

259 d, and Hf isotope composition of kimberlites-volcanic rocks that originate at great depth beneath con

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

261 we examine an extensive compilation of dated volcanic samples from Russia, Mongolia and North China t

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

263 earthquakes (DLPs) are an enigmatic type of volcanic seismicity that sometimes precedes eruptions bu

264 magma storage beneath the depths of located volcanic seismicity.

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

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

267 or accompanied by different types of seismo-volcanic signals.

268 Volcanic SO(2) emission time series reflect magma dynami

269 By scaling to volcanic SO(2) fluxes from a global catalogue, we estima

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

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

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

273 action (>1.6 g/cm(3)) of an unmanaged C-rich volcanic soil caused by lime and/or phosphate applicatio

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

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

276 species combination except H. forsteriana on volcanic soil.

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

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

279 tructed by identifying synchronous (bipolar) volcanic sulfate horizons in Greenland and Antarctic ice

280 A large volcanic sulfate increase observed in ice core records a

281 About 43% more volcanic sulfur is removed from the stratosphere in 2 mo

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

283 ous in erupted products from a wide range of volcanic systems (e.g., Hawai'i, Iceland, Andes).

284 assessing the physical mechanisms of silicic volcanic systems and for constraining deterministic mode

285 e over long timescales, we find that the sub-volcanic systems contain extreme heterogeneity, with mel

286 rusions and the evolution of stresses within volcanic systems is poorly understood, despite its impor

287 but how intrusions are accommodated in other volcanic systems remains unknown.

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

289 such as magnetite during fluid degassing in volcanic systems.

290 nd the evolution and stability of long-lived volcanic systems.

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

292 eres can promote deep convection and trigger volcanic thunderstorms.

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

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

295 rustal-scale fault marked by clusters of non-volcanic tremors directly beneath the southern Central R

296 This is consistent with deep, non-volcanic tremors identified in the same area.

297 ly conducted in granite, clay, saltstone, or volcanic tuff formations.

298 Here we show that along-strike volcanic variability in the Quaternary Cascades Arc is p

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

300 extral transform and rifting in the Northern Volcanic Zone.