ライフサイエンスコーパス: atmospheric

1 Significantly, however, pre-GOE atmospheric aberrations toward more reducing conditions-

2 y calculations involving over half a million atmospheric absorption lines, providing a highly accurat

3 climate with dry and wet seasons and a lower atmospheric abundance of CO2 than is present today.

4 extremely important role in modulating their atmospheric abundance.

5 lobal biogeochemical cycling, and ameliorate atmospheric accumulation of carbon dioxide by 'pumping'

6 on Climate Change, the National Oceanic and Atmospheric Administration, the National Renewable Energ

7 or the elemental carbon (EC) contents in the atmospheric aerosol may have a stronger effect than the

8 Atmospheric aerosol particles (especially particles with

9 he measurement and speciation of cyanides in atmospheric aerosol.

10 O) may incur effects on the SO2 chemistry in atmospheric aerosols because the solvation of SO2 at the

11 (BrC) consists of those organic compounds in atmospheric aerosols that absorb solar radiation and may

12 g can be relatively long-lived components in atmospheric aerosols, thus more likely to have larger im

13 ical behavior of glyoxal at the interface of atmospheric aerosols.

14 ures more closely resembling compositions of atmospheric aerosols.

15 model results indicate an important role for atmospheric aerosols.

16 strong function of combustion efficiency and atmospheric aging.

17 le the standard Sellmeier equation (SSE) for atmospheric air is not intended for the description of a

18 Atmospheric air is still highly transparent to electroma

19 to international trade and the transport of atmospheric air pollution is lacking.

20 ultrashort mid-infrared laser pulses through atmospheric air, probing air dispersion in the 3.6-4.2-m

21 trol has precluded precise alignment of ice, atmospheric and marine records, making it difficult to a

22 duits of terrestrially derived carbon (C) to atmospheric and marine reservoirs.

23 n routes have evolved to exploit predictable atmospheric and oceanic circulation patterns.

24 uture, despite the predicted continuation of atmospheric and oceanic warming.

25 Climatic, atmospheric, and land-use changes all have the potential

26 index value, but which may lead to increased atmospheric baroclinicity and storminess.

27 The precipitous drop in atmospheric black carbon at midcentury reflects policies

28 ts in this region include randomly occurring atmospheric blocking patterns, ocean impacts on atmosphe

29 rine cyclic solutes contradicts a control of atmospheric boron by dissolution of seasalts.

30 During springtime, the Arctic atmospheric boundary layer undergoes frequent rapid depl

31 event on the light absorption properties of atmospheric brown carbon (BrC).

32 the tropics, consistently underestimate the atmospheric burden of CH4 determined via remote sensing

33 cal for simulating stomatal control of plant-atmospheric carbon and water exchange under current, pas

34 nds play an important role in regulating the atmospheric carbon dioxide (CO2 ) concentrations and thu

35 on correlates with a significant drawdown of atmospheric carbon dioxide (CO2) at that time.

36 al variations in the measured growth rate of atmospheric carbon dioxide (CO2) originate primarily fro

37 n over the tropics, while the growth rate of atmospheric carbon dioxide (CO2) was the largest on reco

38 onses to past, present and future changes in atmospheric carbon dioxide concentration ([CO2 ]) is cri

39 anges-especially climate change and elevated atmospheric carbon dioxide concentrations-are increasing

40 ely played an important role in the observed atmospheric carbon dioxide swings by affecting the parti

41 Chemical weathering consumes atmospheric carbon dioxide through the breakdown of sili

42 rby asymmetric-stretch rovibrational band of atmospheric carbon dioxide.

43 We discern the direct incorporation of atmospheric carbon into soil carbohydrate, protein and a

44 centrations can have direct implications for atmospheric carbon sequestration.

45 twentieth century that is based on long-term atmospheric carbonyl sulfide (COS) records, derived from

46 e end of the 21st century as indicated by an atmospheric CH4 and CO2 concentration model.

47 n global surface networks started monitoring atmospheric CH4 mole fractions.

48 e mid-Palaeozoic c. 0.45-0.4 Ga shows global atmospheric changes consistent with increased terrestria

49 rth-like exoplanets that are well suited for atmospheric characterization.

50 nd RBS, respectively) are known for altering atmospheric chemistry and causing sharp tropospheric ozo

51 ir significance in disciplines as diverse as atmospheric chemistry and cell biology.

52 lculations were performed to investigate the atmospheric chemistry of (CF3)2CFCN, a proposed replacem

53 capture literature as well as biological and atmospheric chemistry studies.

54 y clean marine airmasses, each with distinct atmospheric chemistry.

55 droperoxyl radical (HO2) is a key species to atmospheric chemistry.

56 due to a common forcing, such as large-scale atmospheric circulation (North Atlantic Oscillation, NAO

57 ures of the central U.S. linking large-scale atmospheric circulation with the regional climate.

58 ospheric blocking patterns, ocean impacts on atmospheric circulation, and climate's response to anthr

59 idence that a specific pattern of summertime atmospheric circulation--the summer East Atlantic (SEA)

60 rved changes in U.S. frost timing to various atmospheric circulations yielded only modest correlation

61 certainty about how climate change, elevated atmospheric CO2 (atm.

62 productivity by the low partial pressure of atmospheric CO2 (Ca ) experienced during the last glacia

63 nder present and higher partial pressures of atmospheric CO2 (pCO2 = 400 and 1000 ppmv).

64 In Africa and Australia, rising atmospheric CO2 , changing land management and rainfall

65 ferred from double deconvolution analyses of atmospheric CO2 and [Formula: see text]C at different te

66 vironments are warmer, have higher levels of atmospheric CO2 and have altered patterns of disturbance

67 oecosystems that experience rising levels of atmospheric CO2 and O3.

68 stabilizing the increasing concentration of atmospheric CO2 and the global temperature.

69 hnology directly addressing global issues of atmospheric CO2 balance.

70 resulted from elevated N deposition, rising atmospheric CO2 concentration and regional warming.

71 reveals large orbitally driven variations in atmospheric CO2 concentration between [Formula: see text

72 d to underpin much of the ice age decline in atmospheric CO2 concentration, but the specific changes

73 otosynthetic rates at ambient and saturating atmospheric CO2 concentration.

74 in nearly constant proportion to the rise in atmospheric CO2 concentration.

75 Crops grown under elevated atmospheric CO2 concentrations (eCO2) contain less prote

76 Atmospheric CO2 concentrations and nutrient availability

77 ough correlations between the growth rate of atmospheric CO2 concentrations and the El Nino-Southern

78 important role in modulating the changes in atmospheric CO2 concentrations during El Nino events-a p

79 stock grazing, fire-suppression and elevated atmospheric CO2 concentrations facilitating shrub recrui

80 enic carbon dioxide emissions have increased atmospheric CO2 concentrations from 270 to 400 mol mol(-

81 ibution of deforestation emissions to rising atmospheric CO2 concentrations is poorly quantified.

82 acity of land ecosystems to slow the rise in atmospheric CO2 concentrations may be smaller than previ

83 l soils could undergo N-dependent changes as atmospheric CO2 concentrations rise, having global-scale

84 sed to characterize the response of tropical atmospheric CO2 concentrations to the strong El Nino eve

85 vity is most strongly associated with rising atmospheric CO2 concentrations using yearly aggregated d

86 siological responses of plants to changes in atmospheric CO2 concentrations, and fire, as well as wha

87 osystem-scale responses to future changes in atmospheric CO2 concentrations, and thus feedbacks to cl

88 from intact vegetation patches under varying atmospheric CO2 concentrations.

89 iment records suggest that episodes of major atmospheric CO2 drawdown during the last glacial period

90 Rising levels of atmospheric CO2 frequently stimulate plant inputs to soi

91 the synthesis of renewable bioproducts from atmospheric CO2 Growth and metabolism of cyanobacteria a

92 agricultural soils can sequester significant atmospheric CO2 has been questioned.

93 impose restrictions on the potential role of atmospheric CO2 in inferred warmer conditions and valley

94 The abundance variations of near surface atmospheric CO2 isotopologues (primarily (16)O(12)C(16)O

95 owing consensus that the ongoing increase in atmospheric CO2 level will lead to a variety of effects

96 Increases in atmospheric CO2 levels and associated ocean changes are

97 ons rises dramatically by a factor of 2-4 at atmospheric CO2 levels of >220 ppm.

98 Changing atmospheric CO2 levels, climate, and air humidity affect

99 Elevated atmospheric CO2 may widen the disparity in protein intak

100 ven the low levels and large fluctuations of atmospheric CO2 These findings highlight the importance

101 ane seep field on the Svalbard margin reveal atmospheric CO2 uptake rates (-33,300 +/- 7,900 mumol m(

102 changes in Earth's orbital parameters and in atmospheric CO2 using a coupled climate model.

103 Statistical models indicated that increasing atmospheric CO2 was the most important factor driving th

104 Large amplitude variations in atmospheric CO2 were associated with glacial termination

105 hanistically predict gS and A in response to atmospheric CO2, water availability, and time is critica

106 al sea level changes, volcanic degassing and atmospheric CO2, which may have modulated the climate sy

107 We hypothesize that rising atmospheric [CO2] and/or changes in biomass allocation m

108 and growth responses to changing climate and atmospheric [CO2] in the boreal forest.

109 to reactions with halogen atoms, influencing atmospheric composition and pollutant fate.

110 Atmospheric composition varies strongly with altitude wi

111 response of isoprene emission to changes in atmospheric composition.

112 rth system process that alters ecosystem and atmospheric composition.

113 ntreal Protocol has led to reductions in the atmospheric concentration of many ozone-depleting gases,

114 tal complexity associated with assessing OPE atmospheric concentrations across a large urban landscap

115 Rising atmospheric concentrations of CO2 and O3 are key feature

116 f the surface of black phosphorus (BP) under atmospheric conditions is a significant constraint on th

117 varied between experiments; edaphic and mean atmospheric conditions were held constant.

118 However, under atmospheric conditions, the response of wild-type AvLOx

119 late nitrate to be quantified under variable atmospheric conditions.

120 16th-18th centuries) via persistent, blocked atmospheric conditions.

121 anide as an electron mediator under argon or atmospheric conditions.

122 Carbon dioxide is Mars' primary atmospheric constituent and is an active driver of Marti

123 The age-depth relationships show that atmospheric contamination by trace metals (Ag, Cd, Sb, T

124 w the surface which shows that the zenith of atmospheric contamination occurred in the past.

125 vel at 60min (slower glycemic response) than atmospheric counterparts ( approximately 98.3% degree of

126 sources and processes that control the boron atmospheric cycle.

127 n those for PBDEs are consistent with faster atmospheric degradation of PAHs.

128 improving plant performance through reduced atmospheric demand and conservation of available soil wa

129 The data set was compiled by the Delaware Atmospheric Deposition Network (DADN) from samples taken

130 se sites were primarily driven by changes in atmospheric deposition.

131 ter diffusive fluxes greatly overwhelmed the atmospheric depositional flux to the river.

132 nt oxidants and reactants in surface waters, atmospheric drops, and snowpacks.

133 The importance of VPDant suggests that atmospheric drought is important for predicting GPP unde

134 concentrations and isotopic compositions of atmospheric dust and dissolved depositions were monitore

135 habitable in such environments and how their atmospheric dynamics is influenced by the rapidly changi

136 Trends in atmospheric emissions of Hg suggest that local sources a

137 aces, suggesting formation in a low-density (atmospheric) environment.

138 igration of GJ 436b could have triggered the atmospheric escape that now sustains its giant exosphere

139 or (ii) external water and carbon fluxes and atmospheric feedbacks.

140 Much of the atmospheric flux probably derives from emissions from th

141 Local atmospheric forcing therefore plays an important role in

142 nge and can be attributed, in large part, to atmospheric forcing.

143 environments, but their contribution to the atmospheric formation of secondary organic aerosol (SOA)

144 Thus, a large fraction of Mars' atmospheric gas has been lost to space, contributing to

145 Atmospheric gas molecules, particularly water vapour, ha

146 istent with a Rayleigh-like evolution of the atmospheric gaseous boron reservoir with possible but li

147 le to reconstruct the first millennial-scale atmospheric GEM concentration record.

148 ng peat-derived GEM dry deposition to modern atmospheric GEM levels we are able to reconstruct the fi

149 -air methane flux always increase the global atmospheric greenhouse gas burden.

150 ay become more frequent in coming decades as atmospheric greenhouse gas concentrations rise, but the

151 The paleoclimatic sensitivity to atmospheric greenhouse gases (GHGs) has recently been su

152 5) can affect the surface energy balance and atmospheric heating rates and thus may impact the intens

153 oxy for metallicity, we measured HAT-P-26b's atmospheric heavy element content ([Formula: see text] t

154 s appear to be driven by decreasing regional atmospheric Hg emissions although they may be partly cou

155 ear, consistent with the decline in regional atmospheric Hg emissions and water Hg concentrations.

156 al mercury (Hg) have substantially increased atmospheric Hg levels during the 20th century compared t

157 owever, the impact of concomitant changes in atmospheric humidity and CO2 concentration through their

158 HONO is a major source of atmospheric hydroxyl radical (OH), which impacts air qua

159 d 29 s after the event onset in 171 A by the Atmospheric Imaging Assembly/Solar Dynamics Observatory.

160 Atmospheric inputs are the main sources of pollution for

161 ioaccumulation modeling forced by changes in atmospheric inputs reasonably capture magnitudes and tem

162 Model results suggested atmospheric inputs to account for 34-59% ( approximately

163 series allows the determination of the boron atmospheric inputs to this forest ecosystem and contribu

164 e-receptor relationships and by the means of atmospheric inversion we were able to quantify spatially

165 By performing atmospheric inversions, we find evidence of an increase

166 erize the stellar wind of TRAPPIST-1 and the atmospheric ion escape rates for all of the seven planet

167 ar regions, and typical for the near-surface atmospheric layers of Mars.

168 ielding effects can substantially extend the atmospheric lifetime of reactive pesticides from a few d

169 emissions cease altogether, despite the 10-y atmospheric lifetime of this gas.

170 We focus on the amount of atmospheric loss and on the possible biological damage s

171 condensation nuclei for the condensation of atmospheric low-volatile organic compounds.

172 methane emissions have been quantified using atmospheric measurements to provide an independent compa

173 ns affect the sensitivity of Arctic lakes to atmospheric mercury contamination.

174 alt-induced chemical cycling of Hg (through 'atmospheric mercury depletion events', or AMDEs) and wet

175 blished data showing latitudinal declines in atmospheric mercury deposition in Canada, we observed lo

176 o quantify mercury emissions on the basis of atmospheric mercury measurements conducted at the remote

177 Wetlands are the largest global source of atmospheric methane (CH4), a potent greenhouse gas.

178 hyl chloroform, and the C(13)/C(12) ratio in atmospheric methane (delta(13)CH4) from 1983 through 201

179 l wetlands, which are an important source of atmospheric methane.

180 day, water column photosynthesis based on an atmospheric model of spectral radiation, satellite-deriv

181 Using atmospheric model simulations, we show that although cur

182 in the transmission spectrum, together with atmospheric modelling, then gives clues to the propertie

183 ins poorly understood and unaccounted for in atmospheric models.

184 over the rainforest, which strongly enhances atmospheric moisture inflow from the Atlantic.

185 missions) and top-down approaches (measuring atmospheric mole fractions and isotopes) for constrainin

186 SAM chamber (French acronym for "Chamber for Atmospheric Multiphase Experimental Simulation").

187 ting evidence indicates that future rates of atmospheric N deposition have the potential to increase

188 of N availability were independent of recent atmospheric N deposition rates, implying a minor role fo

189 change suggests that, by 2010, anthropogenic atmospheric N deposition represented 20 +/- 5% of the an

190 ignals increased deposition of anthropogenic atmospheric N on the open ocean and its incorporation in

191 erial synthesis to distributed monitoring of atmospheric nanoparticles.

192 hange, the processes and rates of subsurface/atmospheric natural gas exchange remain uncertain.

193 ium symbioses, specialised soil bacteria fix atmospheric nitrogen in return for carbon.

194 relationships with Rhizobium bacteria to fix atmospheric nitrogen.

195 Although increasing atmospheric nitrous oxide (N2O) has been linked to nitro

196 ett and Strawn gas have distinct crustal and atmospheric noble gas signatures, allowing clear identif

197 iable underestimation of the traffic related atmospheric NOx input in Europe, comparable to the weeke

198 ly oxidized organic compounds in maintaining atmospheric NPF.

199 endent on lithology and the concentration of atmospheric O2 Future work on glaciation-weathering-carb

200 eninsula has been widely debated in light of atmospheric/oceanic warming and increases in glacial mel

201 es have implications as key intermediates in atmospheric, organic, and enzymatic reactions.

202 established by depth-dependent variations in atmospheric oxidant and dissolved-solute concentrations.

203 eo-records with which to constrain levels of atmospheric oxidants during past climate transitions.

204 ary organic aerosol (SOA) is formed from the atmospheric oxidation of gas-phase organic compounds lea

205 For TMAO, the potential source is the atmospheric oxidation of marine derived trimethylarsine.

206 Independent of atmospheric oxygen concentration calculated EE has the s

207 during the early stages of the first rise in atmospheric oxygen on the Earth (the Great Oxidation Eve

208 The first significant buildup in atmospheric oxygen, the Great Oxidation Event (GOE), beg

209 which might have helped trigger the rise in atmospheric oxygen.

210 arth's biogeochemical cycles and the rise of atmospheric oxygen.

211 s surface environment, including the rise of atmospheric oxygen.

212 e apparent lag of animal diversification and atmospheric oxygenation during this critical period of E

213 oth size and mass based metrics is common in atmospheric particle measurements, but now, the NTA can

214 Dicarboxylic acids play a key role in atmospheric particle nucleation.

215 Atmospheric particles are notorious for their effects on

216 Organic carbon in atmospheric particles comprises a large fraction of chro

217 n (PMF) was used for apportioning sources of atmospheric particles in late fall in Innsbruck.

218 rticles (core-shell morphology), and ambient atmospheric particles.

219 ssil fuels, and it is a major contributor to atmospheric particulate matter known to have a deleterio

220 nment of water column inorganic arsenic into atmospheric particulates.

221 sent a single response to a rapid decline in atmospheric pCO2 at the EOT.

222 A large and rapid drop in atmospheric pCO2 has been proposed as the driving force

223 otential influence of silicate weathering on atmospheric pCO2 levels on geologically short timescales

224 gress in atmospheric plasmas has led to cold atmospheric plasma (CAP) devices with ion temperatures c

225 Cold atmospheric plasma (CAP), a novel promising anti-cancer

226 Recent progress in atmospheric plasmas has led to cold atmospheric plasma (

227 ing leaf deposited particles as indicator of atmospheric PM concentration and composition.

228 acerifolia is highly suitable to be used in atmospheric PM monitoring studies and that morphological

229 ter than those associated with long-distance atmospheric pollutant transport.

230 produced in the oxidation of a prototypical atmospheric pollutant, n-hexane.

231 Atmospheric pollutants and meteorological conditions are

232 CO2) concentration, and atmospheric pollutants will impact carbon sequestration

233 Particulate matter (PM) in atmospheric pollution contains readily measurable concen

234 Currently one of the main sources of atmospheric pollution identified in urban centers is der

235 Biomagnetic monitoring of atmospheric pollution is a growing application in the fi

236 Atmospheric pollution is largely below the recommended t

237 Atmospheric pollution measurements (nitrogen oxides and

238 Atmospheric pollution was monitored at different sites:

239 ded to increase with first-trimester average atmospheric pressure (odds ratio per 5-mbar increase = 1

240 and aperture from ICT analysis performed at atmospheric pressure are higher than those calculated fr

241 peseed oil under vacuum at 125 degrees C and atmospheric pressure at 165 degrees C.

242 ainst both electrospray ionization (ESI) and atmospheric pressure chemical ionization (APCI) for the

243 urate mass (HRAM) mass spectrometry (MS) and atmospheric pressure chemical ionization (APCI) MS were

244 The novel atmospheric pressure chemical ionization (APCI) source h

245 the sampled materials into the gas phase for atmospheric pressure chemical ionization and mass spectr

246 of a solution of polymer into the commercial atmospheric pressure chemical ionization source on this

247 applied was direct liquid injection into an atmospheric pressure chemical ionization source, followe

248 ently integrates sampling/sample cleanup and atmospheric pressure ionization, making it an advantageo

249 lective hydrocarboxylation of styrenes under atmospheric pressure of CO2 has been developed using pho

250 of solvent or dopant effects as observed in atmospheric pressure photoionization (APPI) and laser io

251 e used in parallel for (1)D detection, while atmospheric pressure photoionization (APPI) MS and ESI-M

252 stionization is achieved in both cases using atmospheric pressure photoionization (APPI).

253 ance of a new orthogonal geometry field-free atmospheric pressure photoionization (FF-APPI) source wa

254 The laser ablation atmospheric pressure photoionization (LAAPPI) and LDTD-A

255 g are two known forms of naturally occurring atmospheric pressure plasmas.

256 iotic CO2 uptake in arid and semiarid soils: atmospheric pressure pumping, carbonate dissolution, and

257 ties and volatilities in different phases at atmospheric pressure remains a challenge.

258 In an atmospheric pressure surface barrier discharge the inher

259 The activation energy values at atmospheric pressure were 548.6kJ/mol and 324.5kJ/mol re

260 cles at elevated temperature under oxygen at atmospheric pressure, by using advanced in situ electron

261 as to novel environmental challenges of low atmospheric pressure, high ultraviolet radiation, and un

262 grow only during periods of relatively high atmospheric pressure, suggesting a formation timescale o

263 n contrast, FAIMS devices operate at or near atmospheric pressure, which complicated integration with

264 t for an increase in preterm birth risk with atmospheric pressure.

265 Treatment of Ni(0) complexes 1a-e with sub-atmospheric pressures of trifluoroethylene (TrFE) afford

266 T-1-makes possible in-depth studies of their atmospheric properties with present-day and future astro

267 ow-cost approach based on the application of atmospheric radio frequency glow discharge (rf-GD) optic

268 isotopic ratios (up to 50 times the present atmospheric ratio, Ra) compared to the lower (3)He/(4)He

269 ch it can be currently detected in different atmospheric regions.

270 cal fluctuations, such as internal tides and atmospheric-related inertial currents, rather than day-n

271 , our measurements suggest that large future atmospheric releases of methane from old carbon sources

272 tude of the ENSO forcing, these sub-seasonal atmospheric responses cannot be detected for moderate El

273 presence of high-amplitude quasi-stationary atmospheric Rossby waves within a particular wavelength

274 Differences in atmospheric samples were generally not as pronounced how

275 y the CH4 flux from the SJB using continuous atmospheric sampling from aircraft collected during the

276 Using global atmospheric simulations with a spatial resolution of 7 k

277 This study uses large-ensemble atmospheric simulations with prescribed ocean surface co

278 module ORACLE to predict the phase state of atmospheric SOA.

279 viding a sink of mesoscale eddy energy as an atmospheric source.

280 HONO chemical formation pathways, as well as atmospheric sources and chemistry.

281 A "jumping" of the PBDE local atmospheric stocks from the Northwestern European Medite

282 We report on a new method for analyzing atmospheric submicrometer particulate organic matter whi

283 The AMO warm SST anomaly generates an atmospheric teleconnection to the North Pacific, which w

284 cean-AIS feedbacks were controlled by global atmospheric teleconnections.

285 , but most likely it is related to increased atmospheric temperature and precipitation, associated wi

286 an be interpreted as a direct consequence of atmospheric temperature differences.

287 dels find that ice nucleated and grown under atmospheric temperatures is at all sizes stacking-disord

288 Molecular hydrogen (H2 ) is an atmospheric trace gas with a large microbe-mediated soil

289 late matter (PM2.5) pollution as a result of atmospheric transport and the production and consumption

290 wever, in contrast to the Arctic, long-range atmospheric transport is deemed less important than huma

291 We apply a high-resolution atmospheric transport model to simulate data from these

292 tial-temporal variability and the long-range atmospheric transport potential of the studied POPs.

293 However, short data records and atmospheric variability confound the search for early si

294 ntic Oscillation (NAO), the dominant mode of atmospheric variability in the Atlantic domain.

295 trees subjected to precipitation reduction, atmospheric warming, and to both simultaneously.

296 le to catastrophic collapse even with little atmospheric warming.

297 llite records, that increased cloudiness and atmospheric water vapor in winter and spring have caused

298 t be attributed to mobile protons donated by atmospheric water.

299 This invariant demonstrates that ocean and atmospheric waves share fundamental properties with topo

300 The initial isotopic composition of atmospheric Xe remains unknown, as do the mechanisms inv