ライフサイエンスコーパス: water vapor

1 tant distance of 1.3 eV from the position of water vapor.

2 ons and in the presence of 3 x 10(17) cm(-3) water vapor.

3 inherently associated with a large efflux of water vapor.

4 y and thus extremely sensitive to changes of water vapor.

5 meworks with unusually high stability toward water vapor.

6 eaction rates between other sCIs and SO2 and water vapor.

7 .6 mm and 0.5 mm wavelengths, and spectra of water vapor.

8 ctures (EWNS) produced by electrospraying of water vapor.

9 either in the absence or in the presence of water vapor.

10 ymer is hardly affected by the adsorption of water vapor.

11 their performance under the condensation of water vapor.

12 atalyst test bench including the presence of water vapor.

13 t from the greenhouse effect of precipitable water vapor.

14 ponse is observed with other gases including water vapor.

15 recipitation)) that depends on the source of water vapor.

16 quantitative spikes of Hg(0), HgBr2, O3 and water vapor.

17 and increased reaction rate with atmospheric water vapor.

18 microwave, irreversible electroporation, and water vapor.

19 nuclei to begin condensation of atmospheric water vapor.

20 mately 100 ppb ammonia in air saturated with water vapor.

21 UST-1 due to its relative instability toward water vapor.

22 rent relative humidities (3, 10, 20, 40%) of water vapor.

23 iation of solid POM salts in the presence of water vapor.

24 raction of convection with free tropospheric water vapor.

25 ion of indoor NO gas, even in the absence of water vapor.

26 igh contrast by exposure to trace amounts of water vapor.

27 opic composition of the source gas CO(2) and water vapor.

28 between environmental changes in oxygen and water vapor.

29 250 degrees C in the presence of oxygen and water vapors.

30 In this work, molecular details of water vapor (0.0-19.0 Torr; 0-96% relative humidity at 2

31 a regulate the uptake of CO2 and the loss of water vapor [1] and contribute to the control of water-u

32 High water vapor (~26 600 ppm) and CO2 concentrations (~4500

33 IR spectra to the absolute positions of the water vapor absorption bands.

34 ions show a spectrum with strong methane and water-vapor absorption.

35 ssue in cloud physics, as the uncertainty in water vapor accommodation on droplets is considerably le

36 technology that uses low-grade heat to drive water vapor across a microporous hydrophobic membrane.

37 organic framework (MOF) thin films to detect water vapor across a wide concentration range is demonst

38 Gradients in the concentration of water vapor across the root system were as small as 10(-

39 f the upper troposphere and the transport of water vapor across the tropopause.

40 and Au-Pd-xCoO nanocatalysts resulting from water vapor addition was due to the formation and accumu

41 Solar irradiance provides energy to desorb water vapor adsorbed to desiccants and determines maximu

42 IX-14-Cu-i were observed to exhibit negative water vapor adsorption at ca. 40-50% relative humidity (

43 y elemental analysis, immersion calorimetry, water vapor adsorption, and Boehm titration.

44 In particular, water vapor adsorption--movement of atmospheric water va

45 by the large number (thousand) of conducted water vapor adsorption-desorption cycles.

46 e spiking delivery for Hg(0), HgBr2, O3, and water vapor after dilution in the manifold ranged up to

47 Vegetation and atmospheric water vapor also had a profound influence on the LST cha

48 ate amine quantifications in the presence of water vapor, ammonia, and CO2 become feasible after prop

49 and predict maximum stomatal conductance to water vapor (Anatomical g(smax)) for individuals.

50 f the wintertime greenhouse effect caused by water vapor and cloudiness has advanced the time of onse

51 t sustains the current levels of atmospheric water vapor and clouds via feedback processes that accou

52 Although KO(2) reacts with water vapor and CO(2) to form KHCO(3) , it is highly sta

53 Akin to open pore materials, water vapor and CO2 gas are shown to be taken up by sing

54 ing barriers for adsorption and diffusion of water vapor and CO2 in the fluorinated and nonfluorinate

55 hange kinetics has allowed the rates of gas (water vapor and CO2) sorption to be quantified by single

56 emporal coupling of changes in temperatures, water vapor and downward longwave radiation (DLR), indic

57 is the process by which liquid water becomes water vapor and energetically this accounts for much of

58 Landscapes influence precipitation via the water vapor and energy fluxes they generate.

59 nges to the biosphere-atmosphere exchange of water vapor and energy of these crops are likely to have

60 dditional mechanism through transpiration of water vapor and feedbacks from the ocean and sea-ice.

61 In addition to being a conduit for water vapor and gas exchange involved in transpiration a

62 wave forcing drives increases in atmospheric water vapor and global precipitation, enhances greenhous

63 Near-infrared absorbance attributed to water vapor and ice and ultraviolet emissions attributab

64 open new perspectives for remote sensing of water vapor and ice in the upper troposphere.

65 and Langmuir constant (k(L)) > 0.1 to adsorb water vapor and meet these maximum potentials.

66 occurs within the combustion reactor between water vapor and molecular oxygen so that only hydrogen i

67 lled around 6 times faster under exposure to water vapor and over 2 times faster when fluorine gas wa

68 In the dark, the continual supply of both water vapor and oxygen is the key factor retaining the a

69 timescale is only 20 y because of robust SW water vapor and surface albedo feedbacks.

70 f the propensity of the frameworks to adsorb water vapor and the proximity of the adsorbed water mole

71 here the air is very sensitive to changes in water vapor and thus efficient in enhancing the longwave

72 articular, materials must be tolerant to the water vapor and to the acidic impurities that are presen

73 ed thin film of the COF responded quickly to water vapor and was stable for months.

74 The maximum total water vapor and water ice within the instrument field of

75 stituted Criegee intermediate (CH3)2COO with water vapor and with SO2 were directly measured via UV a

76 on the surface tension and contact angle of water/vapor and oil/gas systems, by which the capillary

77 e in the vertical lapse rate of temperature, water vapor, and clouds in the troposphere and albedo of

78 spheric circulation patterns and atmospheric water vapor, and find extremely high statistical confide

79 in other climate fields such as atmospheric water vapor, and it is evident in observed temperatures

80 G enhanced the thickness and permeability to water vapor, and made the films more hydrophilic.

81 sive presence and absence of UV irradiation, water vapor, and oxygen were conducted to characterize s

82 of driest quarter, annual mean temperature, water vapor, and precipitation during the coldest quarte

83 hydrophobic surface is exposed to condensing water vapor, and the contaminants are autonomously remov

84 croporous carbon materials in the absence of water vapor, and the hydrated graphite was found to hind

85 with more sustained results with the use of water vapor annealing and layering during device fabrica

86 tions were studied, including silk layering, water vapor annealing and methanol treatment to stabiliz

87 ained release was obtained for 31 days using water vapor annealing.

88 Atmospheric soundings of temperature and water vapor anomalies support the results of the long-te

89 Their interactions with water vapor are particularly relevant in these contexts.

90 w it has been assumed that the blood and the water vapor are the only sources of water to maintain wa

91 hich the escaping MeBr and the generated HBr/water vapors are the main driving forces for circulation

92 WCF), aerosol optical depth and precipitable water vapor as well as global coupled climate models to

93 ) on soybean canopy-scale fluxes of heat and water vapor, as well as water use efficiency (WUE), at t

94 The reversible capture of water vapor at low humidity can enable transformative ap

95 PDMAEMA, there is an apparent enrichment of water vapor at the polymer/air interface.

96 test the hypothesis that the discovery of a water vapor aurora in December 2012 by local hydrogen (H

97 ganized and dense morphology (E-SEM), higher water vapor barrier, better mechanical features (strengt

98 e characterized according to the mechanical, water vapor barrier, thermal, and biodegradability prope

99 the reactions of Criegee intermediates with water vapor, because of high water concentrations in the

100 Atmospheric water vapor binding to soils is a key process driving wa

101 igate the control of flow direction around a water vapor bubble using the thermoplasmonic effect of a

102 pot on the GNF immersed in degassed water, a water vapor bubble with a diameter of ~10 mum is generat

103 d lower loadings below approximately 10 Torr water vapor but greater loadings above this value than s

104 ence of precipitation, absorption of dew and water vapor by litter in the field enables microbial deg

105 followed by optical isotopic analysis of the water vapor by off-axis integrated cavity output spectro

106 Additionally, water vapor can also occupy the roughness valleys of imm

107 ere at current climate temperatures, whereas water vapor can and does.

108 Results show that the increase in water vapor can be largely attributed to human activitie

109 tanding the underlying causes of atmospheric water vapor change is vital in climate change research.

110 he case of the Cu thin film (10 times during water vapor coinjection and 510 times when using a fluor

111 stratosphere, which, in turn, would increase water vapor concentration causing additional ozone loss

112 article ozonolysis found that an increase in water vapor concentration led to lower concentrations of

113 An increase in water vapor concentration led to strong enhancement of g

114 erized at ambient pressure and ten values of water vapor concentration, from 1.0 x 10(2) to 1.7 x 10(

115 Stratospheric water vapor concentrations decreased by about 10% after

116 ting solvent vapour could prevent or disrupt water vapor condensation onto the electrospinning jet; t

117 y component of the climate system, form when water vapor condenses upon atmospheric particulates term

118 If water vapor condenses, that too leads to invasion.

119 d to lead to a large increase in atmospheric water vapor content and to changes in the hydrological c

120 ly evolving free atmospheric temperature and water vapor content are known to be first-order controls

121 Moreover, the increase in atmospheric water vapor content in the Arctic region during late aut

122 s using higher long-term average atmospheric water vapor content than present values.

123 bicity, in terms of the ambient pressure and water vapor content.

124 tently increase more slowly than atmospheric water vapor content.

125 oportionately to the increase in atmospheric water vapor content.

126 C, photoionization detectors, and need-based water-vapor control, we enable sensitive and selective m

127 The observed presence of water vapor convectively injected deep into the stratosp

128 and XRPD studies support our hypothesis that water vapors could trigger the AITC release from these M

129 Here, we examine whether water vapor D&A results are sensitive to model quality.

130 controlled by the delta(18)O of atmospheric water vapor (delta(18)O(a)), and observed delta(18)O(L)

131 ranspiration by affecting carbon dioxide and water vapor diffusion across leaf surfaces, and these tr

132 this inherent coupling of carbon dioxide and water vapor diffusion.

133 electrode does not, as it is covered with a water-vapor diffusion barrier ~8 nm of Al(2)O(3).

134 ents of the evolving isotopic composition of water vapor during cirrus formation experiments in a clo

135 nificantly affected (<3% change at 450 K) by water vapor during solution-aerosol sample introduction.

136 evealed what may prove to be the ubiquity of water vapor during the early stages of planet formation.

137 alkyl groups and framework stability toward water vapor emerges.

138 rtionment of urban emissions, and imply that water vapor emissions associated with combustion may be

139 heories predict a water ice-rich mantle, and water vapor emissions have been observed, yet no water (

140 ird of this feedback comes from increases in water vapor entering the stratosphere through the tropic

141 ayer, with the rest coming from increases in water vapor entering through the extratropical tropopaus

142 Simultaneously, the water vapor evolved from the mineral sample is analyzed

143 The water vapor feedback also inherits diversity from the co

144 ins uncertainties in polar regions while the water vapor feedback spread explains uncertainties elsew

145 mate generally possesses a weaker (stronger) water vapor feedback, yielding a weaker (stronger) warmi

146 e, implying the existence of a stratospheric water vapor feedback.

147 We demonstrate that cloud and water vapor feedbacks in a global climate model compensa

148 ert amplification results from the strongest water vapor feedbacks near the surface over the driest d

149 al pattern of global warming associated with water vapor feedbacks over land in low- and mid- latitud

150 ert amplification might involve two types of water vapor feedbacks that maximize respectively in the

151 ng the inter-model spreads of ice-albedo and water vapor feedbacks, and better understanding the spat

152 We find that estimates of an anthropogenic water vapor fingerprint are insensitive to current model

153 ion of low-adhesion impact behavior and fast water vapor formation supports continuous bouncing and t

154 present here a simple mechanism showing how water vapor forms in situ and is capable of shielding it

155 se sorbent to concurrently extract CO(2) and water vapor from ambient air.

156 An increase in water vapor from near zero to 70% relative humidity (RH)

157 tem and accretion of bright icy particles or water vapor from volcanic plumes originating on the moon

158 Water vapor generation through sunlight harvesting and h

159 of methane (CH(4)), carbon dioxide (CO(2)), water vapor (H(2)O vapor), and hydrogen sulfide (H(2)S).

160 n and climate change on biosphere-atmosphere water vapor (H2 O) and carbon dioxide (CO2 ) exchanges a

161 including molecular oxygen (O2), ozone (O3), water vapor (H2O), carbon dioxide (CO2), nitrous oxide (

162 ion curve of unfunctionalized MOFs caused by water vapor has been established from the temporal compo

163 e cost of synthesis and the stability toward water vapor, have been analyzed and possible solutions a

164 In the presence of water vapor, however, these BINOL networks adsorb less C

165 ed following prolonged exposure to tritiated water vapor (HTO) or tritium/hydrogen gas (HT) in nuclea

166 tudy highlights key mechanisms through which water vapor (i) adsorbs and (ii) condenses at mineral su

167 Through utilizing water vapor in ambient environment as the non-solvent, a

168 apor pressure and hence radiative cooling by water vapor in clear-sky regions.

169 of the ice crystals, modulates the amount of water vapor in ice clouds, and can impact the molecular

170 Stomata control the exchange of CO2 and water vapor in land plants.

171 ensitive detection of 5.1 x 10(-4)% RH/Hz to water vapor in N(2), which is 70 times higher than a dev

172 are likely to be competitive with those with water vapor in polluted urban areas under conditions of

173 le to prepare materials that can convert the water vapor in the air to collectible liquid water is st

174 contribution and fate of combustion-derived water vapor in the atmosphere are lacking, however, and

175 osol particles that contain OS interact with water vapor in the atmosphere.

176 The total abundance of water vapor in the natal habitable zone is equal to that

177 e of ice that grows as a result of uptake of water vapor in the temperature range relevant to cirrus

178 s, that increased cloudiness and atmospheric water vapor in winter and spring have caused an extraord

179 sive drying), this membrane is permeable for water vapor (in case of zeolite 4A permeance = 8 x 10(-9

180 Atmospheric water vapor increases as air temperature rises, which ca

181 The permeance for water vapor increases with increasing pore size of the z

182 s of observations showing that stratospheric water vapor increases with tropospheric temperature, imp

183 vering about 4000 h was performed for phenol-water vapor interacting with four materials pre-equilibr

184 Monitoring phenol-water vapor interactions with the prehydrated sorbents,

185 spectra, the peak origins of water/lipid and water/vapor interfaces are different.

186 been used to probe the isotopically diluted water/vapor interfaces in the spectral regions of OD (22

187 e separation, similar to the condensation of water vapor into droplets.

188 er vapor adsorption--movement of atmospheric water vapor into soil when soil air is drier than the ov

189 electronically excited nitrogen dioxide and water vapor is an important atmospheric source of the hy

190 These findings show that stratospheric water vapor is an important driver of decadal global sur

191 ying how atmospheric particles interact with water vapor is critical for understanding the effects of

192 er-circulation of vapor and brine) occurs as water vapor is driven away from the heat source, condens

193 methylamino)ethyl methacrylate) (PDMAEMA) in water vapor is investigated using a combination of neutr

194 Recent work has suggested that water vapor is likely to be the dominant sink for some C

195 nfluence on observed multidecadal changes in water vapor is not affected by "screening" based on mode

196 lculations show that the catalytic effect of water vapor is not observable at 200-400 K.

197 ducts also shifts to ammonium carbamate when water vapor is present; a new finding that has impact on

198 Water vapor is removed using a heated nafion dryer.

199 on reaction with methanesulfonic acid, (ii) water vapor is required, and (iii) particle formation ca

200 oisture harvesting system is proposed, where water vapor is separated from the air prior to cooling a

201 Our findings suggest potential for water vapor isotope ratio measurements to be used in con

202 uries, only fast climate feedbacks including water vapor, lapse rate, clouds, and snow/sea ice albedo

203 ions change character dramatically near the water vapor-liquid interface.

204 and plants, a fundamental cost of living is water vapor lost to the atmosphere during exchange of me

205 future projections suggest that atmospheric water vapor may increase faster (slower) than that revea

206 ermore, the greenhouse warming by additional water vapor melts sea-ice and triggers a positive feedba

207 The inclusion of the water vapor modifier to the FAIMS methodology is made mo

208 pounds is presented herein with the use of a water vapor modifier.

209 We hypothesized that water vapor molecules could act as an external stimulus

210 CO2 assimilation to stomatal conductance for water vapor) of trees and C3 grassland ecosystems, but t

211 solar-based materials and devices to capture water vapor off the electrical grid have been reported,

212 let formation depends on the condensation of water vapor on ambient aerosols, the rate of which is st

213 studies of the possible catalytic effect of water vapor on CH(3) OH + OH reaction, we report calcula

214 odroplets formed by dropwise condensation of water vapor on low-temperature substrates.

215 lament and the condensation of the resulting water vapor on plasma ions reproduces our experimental f

216 measurements of heterogeneous nucleation of water vapor on silver nanoparticles is presented here us

217 noscale water-in-oil emulsions by condensing water vapor onto a subcooled oil-surfactant solution.

218 ng and is tightly associated with increasing water vapor over deserts.

219 ; humidity levels below approximately 6 g of water vapor per kilogram of air were associated with inc

220 strength (from 22.71 to 3.97 MPa), increased water vapor permeability (from 3.62 to 4.60 g.mm/m(2).da

221 The elongation at break and the water vapor permeability (WVP) values of the films were

222 eable physical properties such as oxygen and water vapor permeability (WVP), swelling, water solubili

223 and more flexible films, with a decrease in water vapor permeability (WVP).

224 and modulus (from 93 to <10 MPa), increased water vapor permeability (WVP, from 3 to 9 g.mm.kPa(-1).

225 AP did not affect the water vapor permeability and tensile strength of the OSA

226 e tensile strength, contact angle, porosity, water vapor permeability and water uptake ratio of CA/Ge

227 The water vapor permeability decreased with increasing MMT c

228 m 5.82 to 2.51 cm(3) um m(-2) d(-1) kPa(-1), water vapor permeability from 1.89 to 1.38 g mm m(-2) h(

229 de-off exists between wetting resistance and water vapor permeability of our monolithic MD membranes.

230 However, the dual modification increased the water vapor permeability of the films without changing t

231 elongation was reduced significantly, while water vapor permeability slightly increased with aging.

232 filmogenic solution increased the thickness, water vapor permeability, and elongation of the films.

233 echanical and barrier properties such as low water vapor permeability, solubility and water holding c

234 ed elongation at break, moisture content and water vapor permeability.

235 relationship between wetting resistance and water vapor permeability.

236 he resulting films' physical, mechanical and water-vapor permeability (WVP) properties were investiga

237 ociated changes in the canopy conductance to water vapor, photosynthetic photon flux density, vapor p

238 It is argued that radiative cooling by water vapor plays an important role in governing the dep

239 rapid decrease with height of the saturation water vapor pressure and hence radiative cooling by wate

240 fic negative effect of drought via increased water vapor pressure deficit.

241 n acid surfaces becomes more negative as the water vapor pressure increases, while it becomes more po

242 adjusting for date, season, temperature, and water vapor pressure on the day of each visit, to estima

243 goethite surfaces subjected to variations in water vapor pressure that are relevant to natural system

244 wly formed ice particles quickly reduced the water vapor pressure to ice saturation, thereby increasi

245 nt pollution and to weather (temperature and water vapor pressure, a measure of humidity).

246 vely associated with ambient temperature and water vapor pressure.

247 en when exposed to elevated temperatures and water vapor pressure.

248 More limited data suggest that stratospheric water vapor probably increased between 1980 and 2000, wh

249 cooling rates where the column precipitable water vapor (PWV) is less than 1 mm.

250 Because electron excitation of water vapor remains the only viable explanation for the

251 oxidation of Sorg(-II)-As(III) complexes in water vapor saturated air over 80 days, monitored by As

252 ts from the nearly exponential dependence of water vapor saturation pressure on temperature, and ther

253 nd-based telescopes, we measured methane and water vapor simultaneously on Mars over several longitud

254 In this study, the water vapor sorption behavior of four nanocellulose samp

255 We report water vapor sorption studies on four primitive cubic, pc

256 r reflectivity using a temperature dependent water vapor source is also described.

257 reactivity of a Criegee intermediate toward water vapor strongly depends on its structure, which wil

258 nly atomizing bulk water but also condensing water vapor, suggesting that spontaneous water oxidation

259 molecules can alter the relationship between water vapor supersaturation and droplet size (i.e., the

260 The coupling of a high partial pressure water vapor system to a conventional X-ray photoelectron

261 lming the effects of decreasing total column water vapor (TCWV) with elevation.

262 aqueous phase and functions as a barrier to water vapor that tempers the effects of humidity changes

263 igh temperatures and spontaneously reacquire water vapor to form aqueous solutions at low temperature

264 The photocatalytic reduction of CO2 by water vapor to produce light hydrocarbons was studied ov

265 icrobial carbon (C) cycling, and the flux of water vapor to soil had a stronger impact than temperatu

266 osed system, we documented the conversion of water vapor to soil liquid water across a temperature ra

267 The simple physical process of adsorption of water vapor to soil particles, forming liquid water, rep

268 By adding (18)O-enriched water vapor to the atmosphere of a closed system, we doc

269 on is almost completely suppressed by adding water vapor to the feed.

270 methods owing to memory effects inherent in water vapor transfer.

271 sults in thickness, opacity, solubility, and water vapor transmission rate (WVTR) analyzes was based

272 Furthermore, the mechanical properties and water vapor transmission rate (WVTR) of the fabricated b

273 e in shelf-life was due to the extremely low water vapor transmission rate of the films, decreasing t

274 other and facilitate the forming of peculiar water vapor transport channel for TRB, which is probably

275 an unexplained by SST were likely due to the water vapor transport dominated by dynamic factors.

276 Simultaneously, intensified water vapor transport from the tropical Pacific and Atla

277 l changes are linked to meridional shifts in water vapor transport from the tropical Pacific toward t

278 which we tentatively attribute to increased water vapor transport into the basin.

279 ng atmosphere result in increased horizontal water vapor transport, bolstering extreme precipitation

280 By calculating the water vapor transport, we suggest instead that different

281 alyzed the relationship among precipitation, water vapor transportation in Tarim River Basin (TRB) an

282 The use of a water vapor trap ensured the accuracy of the results, wh

283 wn to enable exceptionally fast transport of water vapor under a concentration driving force.

284 wn to enable exceptionally fast transport of water vapor under a concentration gradient driving force

285 vimetrical approach to study the kinetics of water vapor uptake from indoor air by silica gel placed

286 polarity is quantified both by its ultrahigh water vapor uptake of 14.3 mmol g(-1) at low relative pr

287 atm and 294 K in the presence and absence of water vapor using an aerosol flow reactor.

288 12 are associated with low CO values and low water vapor values, consistent with transport from the u

289 We show here that stratospheric water vapor variations play an important role in the evo

290 ty using the atmospheric stability factor of water vapor (varphi(w)) calculated from empirical formul

291 Water vapor was generated by pumping a flow of purified

292 ttern of anthropogenically caused changes in water vapor was identifiable with high statistical confi

293 titive adsorption equilibria between VOC and water vapor, which is described by an extended Manes met

294 ints the isotopic signature of stratospheric water vapor, which may allow for a distinction between s

295 However, water vapor will always preferentially adsorb over CO(2)

296 re consistent with two 200-km-high plumes of water vapor with line-of-sight column densities of about

297 The molecular level interactions of water vapor with mineral dust are of global significance

298 s also protect CALF-25 from decomposition by water vapor, with crystallinity and porosity being retai

299 ferential uptake for methane gas relative to water vapor within FMOF-1 pores with ease of desorption

300 tential for interference from ozone (O3) and water vapor (WV), and temporal variability of ambient re