ライフサイエンスコーパス: water vapor

1 .6 mm and 0.5 mm wavelengths, and spectra of water vapor.

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

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

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

5 their performance under the condensation of water vapor.

6 atalyst test bench including the presence of water vapor.

7 t from the greenhouse effect of precipitable water vapor.

8 ponse is observed with other gases including water vapor.

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

10 and increased reaction rate with atmospheric water vapor.

11 microwave, irreversible electroporation, and water vapor.

12 nuclei to begin condensation of atmospheric water vapor.

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

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

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

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

17 raction of convection with free tropospheric water vapor.

18 s and the distribution of upper tropospheric water vapor.

19 sponse from nonacidic organic vapors or from water vapor.

20 dly diluted by large and variable amounts of water vapor.

21 del predictions of the climate feedback from water vapor.

22 estimation of the dilution of RF droplets by water vapor.

23 orcing depends critically on the response of water vapor.

24 molecules than unfolded ones when exposed to water vapor.

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

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

27 inherently associated with a large efflux of water vapor.

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

29 between environmental changes in oxygen and water vapor.

30 meworks with unusually high stability toward water vapor.

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

32 250 degrees C in the presence of oxygen and water vapors.

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

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

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

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

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

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

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

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

41 tively short-circuiting the slower ascent of water vapor across the cold tropical tropopause over the

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

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

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

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

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

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

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

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

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

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

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

53 During boreal summer, much of the water vapor and CO entering the global tropical stratosp

54 Air that is high in water vapor and CO over the Asian monsoon/TP region ente

55 zed guard cells that control the exchange of water vapor and CO(2) between plants and the atmosphere.

56 Removal of water vapor and CO(2) from the air samples prior to trap

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

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

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

60 Extensive isotope exchange between water vapor and crystalline GGV establishes the presence

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

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

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

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

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

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

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

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

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

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

71 It was concluded that the presence of water vapor and post-deposition heat treatment time sign

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

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

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

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

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

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

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

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

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

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

82 fractionation among a few reservoirs of ice, water vapor, and molecular hydrogen on Mars implies that

83 mple organic molecules (HCN, C2H2, and CO2), water vapor, and OH.

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

85 ments with simultaneous aromatic side chain, water vapor, and solvent background subtraction.

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

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

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

89 s, and may help to explain why stratospheric water vapor appears to have been increasing for the past

90 extreme dilution of respiratory droplets by water vapor (approximately 1:12,000).

91 ensors, binary mixtures of solvent vapor and water vapor are correctly classified; following classifi

92 er which conditions ethylene, propylene, and water vapor are not significantly captured while the pre

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

94 surfaces when significant concentrations of water vapor are present.

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

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

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

98 and resistance to oxidation in air with 10% water vapor at 650 degrees and 800 degrees C, were demon

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

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

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

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

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 Any type of sulfur-free gas, including water vapor, can be used to regenerate the sorbent surfa

109 ting over the TP is deeper and detrains more water vapor, CO, and ice at the tropopause than over the

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

111 Water vapor concentration is detected over a range exten

112 Stratospheric water vapor concentrations decreased by about 10% after

113 -HFCV fleet would hardly affect tropospheric water vapor concentrations.

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

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

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

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

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

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

120 tently increase more slowly than atmospheric water vapor content.

121 oportionately to the increase in atmospheric water vapor content.

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

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

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

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

126 tructure and shows increased permeability to water vapor, demonstrating the importance of the cuticle

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

128 er layer of the epidermis, form a barrier to water vapor diffusion through the skin.

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

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

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

132 alkyl groups and framework stability toward water vapor emerges.

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

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

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

136 rosols lead to smaller ice crystals and more water vapor entering the stratosphere.

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

138 traints include the abundance of atmospheric water vapor, escape fluxes of hydrogen and deuterium, D/

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

140 tures that regulate gas (CO(2) and O(2)) and water vapor exchange between plants and their environmen

141 sing measurements of leaf carbon dioxide and water vapor exchange, coupled with modulated chlorophyll

142 The water vapor feedback also inherits diversity from the co

143 quantitative evidence of the reliability of water vapor feedback in current climate models, which is

144 comparing model simulations with and without water vapor feedback, we demonstrate the importance of t

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

152 ic atmosphere caused by photodissociation of water vapor followed by escape of hydrogen to space.

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 s chromatographic columns and for removal of water vapor from product streams were tested.

157 silica films remained hydrophilic and sorbed water vapor from the atmosphere.

158 this paper, we have shown that adsorption of water vapor from the gas phase by magnetoelastic ribbons

159 Water vapor generation through sunlight harvesting and h

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 nteraction between atmospheric particles and water vapor impacts directly and significantly the effec

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

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

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

176 n, including an increase in the abundance of water vapor in the stratosphere (plausibly by as much as

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

178 Water vapor in the tropical and subtropical upper tropos

179 ate models predict that the concentration of water vapor in the upper troposphere could double by the

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

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

182 ts from current climate models indicate that water vapor increases of this magnitude cannot be explai

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

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

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

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

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

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

189 y vibrational spectroscopy was used to study water/vapor interfaces of HCl, HI, and NaOH solutions.

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

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

192 gen isotope data indicates that transport of water vapor into the western Pacific was enhanced during

193 In contrast, water vapor is absorbed by the PDMS to a very minor exte

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

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

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

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

198 ttern of anthropogenically caused changes in water vapor is identifiable with high statistical confid

199 iewed, and the role of dynamic transport and water vapor is identified.

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

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

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

203 The spectrum of water vapor is of fundamental importance for a variety o

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

205 Water vapor is removed using a heated nafion dryer.

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

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

208 measure the gas-phase adsorption behavior of water vapor, isopropyl alcohol, and acetone on a sol-gel

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

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

211 bility and the sensitivity to low background water vapor levels of some platinum(II) double salt mate

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

213 hrough which photosynthetic gas exchange and water vapor loss occur.

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

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

216 e 1.27- and 2.3 micrometers spectra indicate water vapor mixing ratios near 40 +/- 20 parts per milli

217 No large horizontal gradients in the water vapor mixing ratios were detected at these altitud

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

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

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

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

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

223 The effects of water vapor on the cryogenic preconcentration step are q

224 identity, plasma gas flow rate, and residual water vapor on the DBD source performance has been inves

225 r 4 hours, and in the presence or absence of water vapor, on CaP crystallinity was investigated.

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

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

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

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

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

231 The water vapor permeability decreased with increasing MMT c

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

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

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

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

236 can be operated without removal of residual water vapor, permitting it to be directly coupled with c

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

238 osition, and regionally confined nature of a water vapor plume in the south polar region of Enceladus

239 out in situ under near ambient conditions of water vapor pressure (1 Torr) and temperature (275-520 K

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

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

248 emanate from this province, carried aloft by water vapor probably venting from subsurface reservoirs

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 Under proper fracturing conditions, water vapor, resulting from water in the sample and wate

252 water mist in the spark flask, simulating a water vapor-rich volcanic eruption.

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

254 These are the fastest microfabricated water vapor sensors reported to date.

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

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

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

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

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

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

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

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

263 t, without the strong positive feedback from water vapor, the model is unable to reproduce the observ

264 sed to classify binary mixtures of DIMP with water vapor; the PVA/carbon particle composite films are

265 ther demonstrated by their ability to adsorb water vapor to form [Er(2)(PDA)(3)(H(2)O)] x 2H(2)O quan

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

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

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

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

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

271 ted [CO(2)] results in decreased transfer of water vapor to the atmosphere.

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

273 mbient air at the tropopause also allow more water vapor to travel into the lower stratosphere over t

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

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

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

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

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

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

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

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

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

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

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

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

286 12 are associated with low CO values and low water vapor values, consistent with transport from the u

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

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

289 Water vapor was generated by pumping a flow of purified

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

291 Most exhaled water is produced as gaseous water vapor, which can be collected in cooled condensers

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

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

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

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

296 y interest (ethanol, methanol, acetonitrile, water vapors) with a single 13.56-MHz RFID tag coated wi

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

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

299 upled with photochemical reactions involving water vapor would give rise to the sustained production

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