ライフサイエンスコーパス: degassing

1 ocal stability is increasing in the zones of degassing.

2 antle melting, magma ascent and near-surface degassing.

3 essing the fractionation of volatiles during degassing.

4 strial reservoirs, as opposed to rapid early degassing.

5 hane oxidation, and volcanic and metamorphic degassing.

6 rucial geochemical tool for studying Earth's degassing.

7 ad consistent with predicted depths of water degassing.

8 g mantle melting, magma differentiation, and degassing.

9 S) technology to monitor underwater volcanic degassing.

10 centrations of 0.4 to 1.3 wt% CO(2) prior to degassing.

11 ents, which we relate to fluid migration and degassing.

12 ow, deep or transcrustal differentiation and degassing.

13 e explosions separated by periods of passive degassing.

14 and are CO(2)-dominated, even during passive degassing.

15 ponding increase in CO2 inputs from volcanic degassing.

16 ing may also vary due to changes in volcanic degassing.

17 ic eruption, did not experience posteruptive degassing.

18 rdial material never processed by melting or degassing.

19 uitability of 40Ar as a monitor of planetary degassing.

20 er an air atmosphere, obviating the need for degassing, a glovebox, or Schlenk techniques.

21 (11.7 x 10(11) mol CO(2)/y) for non-eruptive degassing and 1.8 +/- 0.9 Tg/y for eruptive degassing du

22 iving magma fragmentation depending on magma degassing and ascent dynamics.

23 between glacial sea level changes, volcanic degassing and atmospheric CO2, which may have modulated

24 Early planetary degassing and atmospheric escape are two major, yet unco

25 ean-ridge basalt magmas, and hence constrain degassing and contamination histories of mid-ocean ridge

26 hod uses a synergistic combination of vacuum degassing and coverslip sweeping.

27 The importance of the interplay between degassing and crystallization before and after the erupt

28 CO2 is heavily influenced by modern volcanic degassing and equilibration with liquid water.

29 -year Earth system response to sudden carbon degassing and global warming episodes.

30 Combined with glucose oxidase for in situ degassing and H(2)O(2) generation, such NIR dye particle

31 c record and is evidence of volcanic halogen degassing and its potential role for the Cretaceous-Tert

32 antle, thereby decreasing the rate of mantle degassing and leaving significant amounts of noble gases

33 mn structure has not been compromised by the degassing and local stability is increasing in the zones

34 (2) in hydrothermal fluids point to magmatic degassing and melt-impregnation as the main source of CO

35 s mixing with non-geothermal waters or H(2)S degassing and oxidation with increasing distance from a

36 epth of 410 to 660 kilometers) unaffected by degassing and shallow crustal contamination.

37 n (~ 30%) and harsh sample treatment such as degassing and sorption cycles.

38 dality, attributed here to episodic volcanic degassing and subsequent oceanic carbonate saturation.

39 gas measurements for detecting heterogeneous degassing and suggests that traditional CO(2) flux measu

40 Degassing and the addition of 2-hydroxyglutarate to the

41 n our understanding of the history of mantle degassing and the evolution of crustal recycling, the re

42 uch fragmentation may be important for magma degassing and the inhibition of explosive behaviour.

43 hermal environments, which involves magmatic degassing and water-consuming mineral reactions occurrin

44 Dome growth and explosive degassing are fundamental processes in the cycle of cont

45 This suggests LIP magma degassing as a primary kill mechanism for mass extinctio

46 al-magma differentiation or daughter-isotope degassing as the main causes for the signal.

47 days before eruptions and that the manner of degassing, as deduced from geochemical signatures within

48 th of these require significant planetesimal degassing, as metamorphic devolatilization on chondrite-

49 nitrogen from the crystalline basement alone-degassing at a steady state in proportion to crustal hel

50 2)S and S(2), are dominantly emitted through degassing at crustal to surficial pressures.

51 The degassing at Fagradalsfjall and our explanatory model th

52 O2 production and thereby to global volcanic degassing at plate boundaries.

53 We simulated volcanic degassing, atmospheric escape, and crustal hydration on

54 l chemical framework for understanding magma degassing, but quantify the primacy of magmatic chlorine

55 Here we quantitatively estimate CO2 degassing by reconstructing lithosphere subduction evolu

56 nger and larger than estimates for the total degassing by the Columbia River Basalt eruptions, implyi

57 d timing of the inferred changes in tectonic degassing can account for the majority of long-term ice

58 However, degassing can impact magmatic fO2 before or during erupt

59 resulting in the precipitation of calcite by degassing CO2, had the unintended consequence of providi

60 Volcanic and metamorphic degassing comprise ~23% of the total C input.

61 ane release with mass mortality and volcanic degassing contributing in secondary roles.

62 esulting in the buildup of CH4, formation of degassing cracks in sediments and an increase in the ben

63 We therefore use our degassing curve as input for the GEOCARBSULF model to es

64 onizing the quantity and quality of magmatic degassing data available and insights into volcanic proc

65 Importantly, where S-degassing does occur, OPB have higher CSE contents than

66 We infer that degassing during decompression of water-saturated magmas

67 es of the lunar magmatism, followed by magma degassing during generation, transport, and eruption of

68 One mechanism for degassing during magma ascent, consistent with observati

69 which were likely formed as a result of CO2 degassing during removal from the deep subsurface (>70m

70 the bulk rock, and instead record localized degassing during the final stages of lunar magma ocean (

71 reached 2.7 Ga ago, implying intense mantle degassing during the first 1.7 billion years of Earth's

72 degassing and 1.8 +/- 0.9 Tg/y for eruptive degassing during the period from 2005 to 2015.

73 y in erupting volcanoes is controlled by the degassing dynamics and the viscosity of the ascending ma

74 nated from the specific dissolution rate and degassing effect of each constitutive compound.

75 So far, such degassing estimates were based on reconstructions of oce

76 n the He isotope ratio, as well as intensive degassing evidenced by fractionated (4)He/(40)Ar(*) valu

77 Areas of diffuse CO(2) degassing exhibit increasing mantle CO(2) flux and (3)He

78 g flux must adjust to equal the volcanic CO2 degassing flux.

79 ications for solid Earth [Formula: see text] degassing fluxes need to be further investigated.

80 Extensive degassing from organic-rich sediments intruded by magmas

81 Our data suggest that volcanic sulfur degassing from such activity could have caused repeated

82 Sicily are regions of intense natural CO(2) degassing from surface seeps.

83 simple isotopic systematics is used to trace degassing from the mantle, to date groundwater and to ti

84 issolved inorganic carbon caused by volcanic degassing, global warming, and sea-level rise.

85 e; thus, it is likely that metamorphic CO(2) degassing has not been constant throughout time.

86 rth's mantle and the influence that magmatic degassing has on the chemistry of the oceans and the atm

87 n is active and ongoing, and recent volcanic degassing has played a substantial role in the compositi

88 elease of large amounts of CO2 from volcanic degassing; (iii) the release of methane stored in methan

89 halogen cycle is characterized by efficient degassing in the early Earth and subsequent net regassin

90 (2), HCl, HF and CO) reveal a stage of CO(2) degassing in the upper crust during magma ascent, follow

91 xide minerals such as magnetite during fluid degassing in volcanic systems.

92 C relative to S is the hallmark of silicate degassing, indicating that parent body core compositions

93 the lunar crust, they were not subjected to degassing into vacuum.

94 Deep Earth degassing is a critical forcing factor for atmospheric C

95 ur dioxide (SO2) emitted by passive volcanic degassing is a key parameter that constrains the fluxes

96 Volcanic degassing is a source of these elements to Earth's surfa

97 t on atmospheric thickness and that volcanic degassing is most efficient for planets between 2 and 4

98 gnificance, an inventory of passive volcanic degassing is very difficult to produce, due largely to t

99 ith higher delta(13)C values (e.g., volcanic degassing) is associated with the long-term LPEE.

100 can affect the environment through volatile degassing, it remains debated what controls the severity

101 s a 12-km wide caldera and several intensely-degassing lava lakes confined to intra-caldera cones.

102 underestimate contributions from cold CO(2) degassing, leading to underestimated global volcanic flu

103 -210 excesses, which signals the presence of degassing magma at depth.

104 tope systematics that support an origin from degassing mantle melts.

105 While solid-Earth degassing may have acted as a trigger, subsequent biotic

106 ed at arc settings, experiencing storage and degassing, may lack such textures due to fundamentally d

107 entrations in slow-flowing anoxic systems as degassing mechanisms are not strong.

108 gas are consistent with a single-stage water degassing model, a two-stage oil modified groundwater ex

109 Conceptual degassing models for quiescent continental crust are dom

110 as the potential to revolutionize underwater degassing monitoring and provide valuable information fo

111 on can neither be explained by modern mantle degassing nor recycling via subduction zones.

112 Here, we show that degassing occurred over a period of decades to days befo

113 itution and can be achieved by simple vacuum-degassing of 4c (R = iPr) to regain 1c.

114 of Saturn, are creating fractures that cause degassing of a clathrate reservoir to produce the plume

115 unar volatiles accreted onto Earth, and from degassing of a differentiating lunar magma ocean, implyi

116 ls, ranging from closed-system extraction to degassing of a wholly molten body, show that significant

117 sses and instead suggest early and extensive degassing of an isotopically light vapor.

118 Degassing of bare cores stripped of their silicate mantl

119 tic melts is important for understanding the degassing of basaltic magma and for assessing the fracti

120 If degassing of basalts were responsible for the rise in ox

121 dely separated sites support the notion that degassing of biogenic methane hydrate may have been an i

122 Changes in the upwelling and degassing of carbon from the Southern Ocean form one of

123 er, little is known about the speciation and degassing of carbon in magmas formed on other planets (i

124 ean crustal production, a proxy for tectonic degassing of carbon, suggests that crustal production ra

125 ved organic carbon to the atmosphere through degassing of central Aleutian volcanoes, while slow and

126 no residual (14)C-depleted signals owing to degassing of CO(2) and biological uptake in the Southern

127 l which considers the impact of LIPs through degassing of CO(2) and enhancement of local continental

128 The degassing of CO(2) supersaturated groundwater following

129 also atmosphere composition through volcanic degassing of CO2 at subduction zones and midocean ridges

130 ed during this seismic cluster records rapid degassing of CO2, suggesting an interval of anomalous fl

131 Our data imply carbon saturation and degassing of Deccan magmas initiated at high pressures n

132 n OIBs than in MORBs leads to more extensive degassing of helium in OIB magmas and that noble gases i

133 r decades, little attention has been paid to degassing of magmatic CO(2) and mineral carbonation of m

134 ater content of the regolith may suggest the degassing of mantle reservoir beneath the Chang'E-5 land

135 of MVEs during condensation of the Moon, and degassing of MVEs during lunar magma ocean crystallizati

136 Volcanic degassing of planetary interiors has important implicati

137 Degassing of planetary interiors through surface volcani

138 e is present and is likely due to incomplete degassing of pre-existing He during the casting process.

139 en more than previous data indicate, and the degassing of reduced carbon from Fe-rich basalts on plan

140 out on the benchtop with no purification or degassing of solvents or reagents, and requires no exclu

141 However, because of eruption-related degassing of sulfur (S) and the compositional, pressure,

142 /(4)He in plumes may thus reflect incomplete degassing of the deep Earth during continent and ocean c

143 Degassing of the Earth's mantle through magmatism result

144 y be explained by disequilibrium open-system degassing of the erupting magma.

145 We also underline that degassing of the sample is important to achieve highest

146 ble riding" by sulfide droplets, followed by degassing of the shallow, sulfide-saturated, and excepti

147 onstrained, numerical modelling of diffusive degassing of the very-low-Ti glasses provides a best est

148 ters, where pits are thought to form through degassing of volatile-bearing material heated by the imp

149 eanic crust carbon to the atmosphere through degassing of western Aleutian volcanoes.

150 theory, originate from contemporary volcanic degassing or chlorine released from gas-solid reactions.

151 om later volatile capture rather than impact degassing or outgassing of the solid Earth during its ma

152 rged a total of 63 kt/day SO2 during passive degassing, or 23 +/- 2 Tg/yr.

153 (22)Ne ratio is sensitive to solar-Ne mantle degassing over geological time.

154 Critical magma degassing parameters are the depth, chemistry and style

155 rust, resulting in a heretofore unrecognized degassing pathway that can accommodate the water subduct

156 While magma degassing plays a clear key role in their generation, th

157 was removed from the precursor by a thermal 'degassing' process.

158 c conduits, which has implications for magma degassing processes and eruptive styles.

159 space can provide key insights into magmatic degassing processes globally, aiding understanding of er

160 0 values in all settings largely result from degassing processes rather than mineral-melt partitionin

161 r consideration of cosmic-ray spallation and degassing processes, our results demonstrate that lunar

162 Intensive degassing produces a gas jet in which locally scavenged

163 cates a large increase in the tectonic CO(2) degassing rate between the Neoproterozoic and Paleozoic

164 Carlo simulations reveal that the volume and degassing rate of CO(2) emissions from the Kerguelen LIP

165 e lower than today (129)Xe excess requires a degassing rate of radiogenic Xe from the mantle higher t

166 ss, thermal state, and age mainly affect the degassing rate.

167 with hypotheses suggesting changes in CO(2) degassing rates or modification of silicate weathering t

168 Our results indicate that degassing rates were anomalously low during the Late Neo

169 ctor of four or more when compared to modern degassing rates, contributing to a stronger greenhouse e

170 iation) periods with implications for mantle degassing rates.

171 in the absence of appreciable changes in CO2 degassing rates.

172 e predict the CO(2)/S(T) gas ratio of 34 top-degassing remote volcanoes with no available gas measure

173 act on surface fO2 We show that low-pressure degassing resulted in reduction of the fO2 of Mauna Kea

174 major difficulties with this simple magmatic degassing scenario--argon seems to be compatible in the

175 Through E-field pre-activation during degassing, several zeolites exhibited enhanced CO(2) ads

176 The vacuum degassing step dislodges air bubbles from the microwells

177 ron X-ray imaging) are mitigated by multiple degassing steps.

178 es and, if necessary, the design of feasible degassing strategies.

179 This implies that the CO(2) degassing style changed as the Siberian Traps emplacemen

180 CO(2) flux from the Earth's 91 most actively degassing subaerial volcanoes at 38.7 +/- 2.9 Mt/yr (or

181 rmation of hexagonal delta-MoN and the onset degassing temperature increases as the pressure increase

182 d NADP(+) increase proportionately; however, degassing the sample and flushing the sample tubes with

183 tes that CoA is labile in solution; however, degassing the sample with helium gas halted its oxidatio

184 series with a gas exchanger and a vessel for degassing the system during filling.

185 t zone of the transform fault and subsequent degassing, the fault constitutes a conduit for CO(2)-ric

186 On degassing, the locked dislocations can be reactivated un

187 d SO(2)/HCl ratios, while during the passive degassing these ratios are lower.

188 Degassing treatment for HOF-30 yields HOF-30a with 3D te

189 Extension of our findings via modeling of degassing trends suggests that a decrease in eruption pr

190 g a cause-effect relationship where volcanic degassing triggers global climatic changes.

191 ucing the air volume circulating through the degassing unit and radon detector are made.

192 bly lower than the commonly assumed volcanic degassing value.

193 ced by magma during ascent strongly controls degassing, vesiculation, magma strength and the effusive

194 n that the atmospheric plumes of quiescently degassing volcanoes are chemically very active, pointing

195 d real-time measurements of large numbers of degassing volcanoes world-wide are now possible, revolut

196 easured, CO(2) emissions from several remote degassing volcanoes worldwide can be predicted using reg

197 n active termite mounds [3] or on the rim of degassing volcanoes, seemingly preferring such hardship

198 Controlled degassing was initiated at Nyos (2001) and Monoun (2003)

199 terrestrial accretion of halogens and mantle degassing, which has removed less than half of Earth's d

200 models, to show that the Noril'sk ores were degassing while they were forming.