ライフサイエンスコーパス: atmosphere

1 he following active phase by stabilizing the atmosphere.

2 lly to the formation of biogenic SOAs in the atmosphere.

3 ols influence solar radiative forcing of the atmosphere.

4 e of carbonaceous aerosol in the terrestrial atmosphere.

5 e partitioning of CO2 between the oceans and atmosphere.

6 s clues to the properties of the exoplanet's atmosphere.

7 rstanding of natural levels of Pb in Earth's atmosphere.

8 that contributes to the iodine burden of the atmosphere.

9 e risk that stored C will be returned to the atmosphere.

10 creased greenhouse gas concentrations in the atmosphere.

11 on source in an argon (Ar) and nitrogen (N2) atmosphere.

12 that typically have extended lifetime in the atmosphere.

13 , warm, wet environment to today's cold, dry atmosphere.

14 e soil-based microbes are transferred to the atmosphere.

15 flow as the source of SVOCs to the island's atmosphere.

16 10,607 Tg C release from land ecosystems to atmosphere.

17 resulting in additional CO2 uptake from the atmosphere.

18 genic carbon dioxide emissions remain in the atmosphere.

19 iologically relevant molecules in a reducing atmosphere.

20 nsport energy from the interior to the outer atmosphere.

21 g priority pollutants in groundwater and the atmosphere.

22 ce waters were in contact with an oxygenated atmosphere.

23 source of atmospheric N2O5 and ClNO2 to the atmosphere.

24 ude of reservoir methane (CH4) fluxes to the atmosphere.

25 ine, inhibiting further interaction with the atmosphere.

26 rescence DCA (DCA-CF), and static controlled atmosphere.

27 n heating up to 600 degrees C under an inert atmosphere.

28 n illumination, at 60 degrees C, and in a N2 atmosphere.

29 lux of plant respired CO2 from leaves to the atmosphere.

30 ents incubated under fluctuating oxic/anoxic atmosphere.

31 o prevent lake waters from being lost to the atmosphere.

32 1) (+/- 2sigma, s.d.) relative to the modern atmosphere.

33 systems, its main natural contributor to the atmosphere.

34 idinium photoredox catalyst under an aerobic atmosphere.

35 deep sea, as well as soaking up CO2 from the atmosphere.

36 s in these wetlands on methane fluxes to the atmosphere.

37 he extent of plant emissions of CH3Cl to the atmosphere.

38 ease large pulses of greenhouse gases to the atmosphere.

39 d source of organic aerosols in the pristine atmosphere.

40 affected forests into a carbon source to the atmosphere.

41 lating the accumulation of carbon (C) in the atmosphere.

42 ollowing a sulfurization treatment in an H2S atmosphere.

43 ed in hexagonal boron nitride under an inert atmosphere.

44 to such increases may be present in Earth's atmosphere.

45 tate (2H) when mildly annealed in a nitrogen atmosphere.

46 hich heat conduction maintains an isothermal atmosphere.

47 r film persisting on the surface under a dry atmosphere.

48 tion and vertical temperature profile of its atmosphere.

49 harged cations to the inner shell of the ion atmosphere.

50 es by denitrification from ecosystems to the atmosphere.

51 nisothermal decomposition of PE in NOx-doped atmosphere.

52 anic eruptions led to the oxygenation of the atmosphere.

53 glaciation may act as a source of CO2 to the atmosphere.

54 otopes to track the evolution of the Earth's atmosphere.

55 derstanding of the complex OA sources in the atmosphere.

56 e gas exchange between the biosphere and the atmosphere.

57 ich release large amounts of pollen into the atmosphere.

58 production and loss mechanisms of BrC in the atmosphere.

59 O2 of 1.9 +/- 0.3 years (upper limit) in the atmosphere.

60 finitely stable at room temperature in inert atmosphere.

61 tive explanations for the oxygenation of the atmosphere.

62 ent (>85% RH) or 6 months of exposure to the atmosphere.

63 nefits in organisms living in an oxygen-rich atmosphere.

64 known source of brown carbon aerosol in the atmosphere.

65 - and long-wavelength-infrared optics of the atmosphere.

66 changes in the greenhouse gas content of the atmosphere.

67 ng particulate organic carbon in the Earth's atmosphere.

68 r quadrillion per volume (ppqv) range in the atmosphere.

69 tile organic compound (VOC) emissions to the atmosphere.

70 nd the subsequent release of CO2 back to the atmosphere.

71 as-phase systems of combustion and planetary atmospheres.

72 ar TRAPPIST-1 are capable of retaining their atmospheres.

73 In both atmospheres, a bimodal apparent activation energy is obs

74 repared in the air, here, using selected gas atmospheres, a large change in the water contact angle o

75 ate of kinetic energy replenishment from the atmosphere above.

76 Under oxic atmosphere, aerobic metabolic VC oxidation was absent in

77 carbon elimination from silicon kerf in two atmospheres: air and N2, under a regime of no-diffusion-

78 ortality and morbidity in Heart Failure) and ATMOSPHERE (Aliskiren Trial to Minimize Outcomes in Pati

79 ortality and Morbidity in Heart Failure) and ATMOSPHERE (Aliskiren Trial to Minimize Outcomes in Pati

80 xygen production and its accumulation in the atmosphere (also known as the Great Oxidation Event) 2.4

81 Hydrogen cyanide is a ubiquitous gas in the atmosphere and a biomass burning tracer.

82 tisfactory results were obtained in modified-atmosphere and air-packaged patties.

83 uld have been present at the base of such an atmosphere and also deeper in the porous crust.

84 a site's gas production to be emitted to the atmosphere and are the defining attribute of super-emitt

85 N2 released from marine ecosystems into the atmosphere and are thus indispensible for balancing the

86 r oxygen is released, maintaining an aerobic atmosphere and creating the ozone layer.

87 Large ocean-atmosphere and hydroclimate changes occurred during the

88 ts the need for an accurate coupling between atmosphere and ice sheet components in climate models.

89 r understand the interactions between ocean, atmosphere and ice sheet stability during the YD, more h

90 g flux between the terrestrial biosphere and atmosphere and infers a residence time of CO2 of 1.9 +/-

91 tic SSTs can trigger diabatic heating in the atmosphere and influence the extratropical climate throu

92 The system couples the atmosphere and land, with moist forest that depends on c

93 d by dust storms are transported through the atmosphere and may affect human health and the functiona

94 Here we analyze atmosphere and ocean observations and identify evidence

95 e orebodies, preventing its release into the atmosphere and oceans.

96 ous chemicals that are still detected in the atmosphere and other environmental media, although their

97 ane released from the seafloor may reach the atmosphere and potentially amplify global warming.

98 lows extraction of new properties of the ion atmosphere and provides an electrostatic meter that will

99 icated by local foregrounds like the Earth's atmosphere and sunlight reflected from local interplanet

100 cting the partitioning of carbon between the atmosphere and the ocean.

101 The existence of the Sun's hot atmosphere and the solar wind acceleration continues to

102 s, possibly leading to large N losses to the atmosphere and to aquatic systems.

103 upper-atmospheric structure made by the Mars Atmosphere and Volatile Evolution (MAVEN) spacecraft.

104 z energy cycle is widely used to investigate atmospheres and climates on planets.

105 ed Hg, 470 Gg were emitted directly into the atmosphere, and 74% of the air emissions were elemental

106 arbors three times as much carbon as Earth's atmosphere, and its decomposition is a potentially large

107 fy its impact on OVOC and SOA burdens in the atmosphere, and ultimately on climate.

108 on is performed at room temperature, open to atmosphere, and without the need to rigorously exclude w

109 life; its vapour and droplets fill the lower atmosphere; and even rocks contain it and undergo geomor

110 a ecosystems were a net source of CO2 to the atmosphere annually, with especially high rates of respi

111 er volumes at the most abundant sizes in the atmosphere ( approximately 100 nm).

112 and anisole to the environment, which in the atmosphere are converted into the respective phenols, cr

113 Human emissions of V to the atmosphere are now likely to exceed background emissions

114 ntial contribution of comets to inner-planet atmospheres are long-standing problems.

115 t abundant volatile organic compounds in the atmosphere, are readily oxidized by ozone.

116 es suggest that the efficiency of the global atmosphere as a heat engine increased during the modern

117 e increase in the capture of carbon from the atmosphere as elemental sulfur is oxidised to sulfate.

118 (PAHs) are widely distributed throughout the atmosphere as mixtures attached to ambient particulate m

119 that is retained in biomass vs. lost to the atmosphere as respiration.

120 nternal pressure as high as approximately 50 atmospheres as a result of the phage DNA-packaging proce

121 fer up the food chain, volatilization to the atmosphere, as well as direct phytotoxic impacts to plan

122 phere is unique among Solar System planetary atmospheres, as its radiative energy equilibrium is cont

123 )4(fumarate)6]} that captures water from the atmosphere at ambient conditions by using low-grade heat

124 reveal the isotopic composition of the paleo-atmosphere at approximately 3.3 Ga.

125 factors that dominate the PCB burden in the atmosphere at both Camden and New Brunswick resemble Aro

126 on mass spectrometry, I2 was observed in the atmosphere at mole ratios of 0.3-1.0 ppt, and in the sno

127 oyed to determine the composition of the ion atmosphere at physiological ionic strength.

128 mo- and chloroxenate salts are stable in the atmosphere at room temperature and were characterized in

129 ared with the sorbent samples in phenol-free atmosphere at the same RH, showed, for the first time, a

130 The total mechanical energy of the global atmosphere basically remains constant with time, but the

131 anthropogenic CO2 emission into the Earth's atmosphere but also produces carbon compounds that can b

132 acids and the effects of the surrounding ion atmosphere, but experimental measures of the potential a

133 s critical sites of methane emissions to the atmosphere, but the biogeochemical reactions driving suc

134 important source of greenhouse gases to the atmosphere, but uncertainties remain in the flux rates a

135 eased the simulated emissions of VOCs to the atmosphere by 28%, including a 2,000-fold decrease in em

136 we have altered the deposition of V from the atmosphere by a similar amount.

137 offset anthropogenic CO2 emissions into the atmosphere by burying this greenhouse gas in the subsurf

138 Ion counting experiments quantify the ion atmosphere by measuring the preferential ion interaction

139 ces are explored for removal of TFA from the atmosphere by reaction with biogenic Criegee intermediat

140 evaluate the interaction between controlled atmosphere (CA), CA+1-methylcyclopropene (1-MCP) and dyn

141 ic carbon (OC) from the short-term biosphere-atmosphere carbon (C) cycle, and therefore prevents gree

142 planet that reduced ionization in the upper atmosphere, causing a north-south asymmetry.

143 leased large amounts of CO2 and CH4 into the atmosphere, causing severe global warming and subsequent

144 d by the atoms and molecules in the planet's atmosphere, causing the planet to seem bigger; plotting

145 ce, but also have significantly altered land-atmosphere CH4 emissions for this region, potentially ac

146 ed CH4 flux is an important pathway for land-atmosphere CH4 emissions, but the magnitude, timing, and

147 The troposphere is the region of the atmosphere characterized by low static stability, vigoro

148 s impacting ecosystem productivity and ocean-atmosphere climate dynamics.

149 ate that oxidative fluxes could change ocean-atmosphere CO2 equilibrium by 25 ppm or more over 10 ky.

150 her improve modeled projections of biosphere-atmosphere CO2 exchange in a changing climate.

151 Experiments in an inert helium atmosphere confirm that FeO reacts via a redox mechanism

152 t simulations were carried out in a reducing atmosphere containing NH3 + CO.

153 The present-day Earth atmosphere contains 22 +/- 5% cometary xenon, in additio

154 Strikingly, quantitation of the ion atmosphere content indicates that divalent cations are p

155 he role of many traits across the soil-plant-atmosphere continuum is then used to establish differenc

156 dia test facility to simulate the soil-plant-atmosphere continuum.

157 The effects of dynamic controlled atmosphere (DCA) storage based on chlorophyll fluorescen

158 'Fuji Suprema' apples, in dynamic controlled atmosphere (DCA), treated with or without 1-methylcyclop

159 insolation, the planet may have retained its atmosphere despite the greater luminosity (compared to t

160 roblem and allow introduction of Ni into the atmosphere during eruption of the SLIP lavas.

161 inor fraction (0.07%) was transferred to the atmosphere during periods of low wind speeds.

162 to 57%) are evaporating and released to the atmosphere during roasting.

163 y have brought this component to the Earth's atmosphere during the last stages of terrestrial accreti

164 primary arc magmas that release gases to the atmosphere during volcanism.

165 transfer of 40-70 Pg carbon from soil to the atmosphere each year.

166 The North Atlantic ocean/atmosphere environment exhibits pronounced interdecadal

167 date key processes controlling the biosphere-atmosphere exchange of H2 and raise new questions regard

168 e summer monsoon, suggesting that local land-atmosphere feedbacks involving desiccated soils and vege

169 C light by oxygen in Archaean earth's anoxic atmosphere followed by chirally selective damage of biom

170 alogs have previously been identified in the atmosphere following spray applications in the states of

171 ed these peatlands into net C sources to the atmosphere for a decade following thaw, after which post

172 uda) were stored in air and under a modified atmosphere for several days after their expiry date and

173 o direct acoustic propagation from the upper atmosphere for which travel time would be several minute

174 em regulation are caused by changes in ocean-atmosphere forcing and triggered by highly variable clim

175 undergone the extreme early loss observed in atmosphere-forming elements.

176 Storage in a regular controlled atmosphere gave higher levels of key volatiles (butyl ac

177 for chemistry occurring in and around urban atmospheres globally.

178 We find that the periodic forcing of the atmosphere has a noticeable impact on the planet's clima

179 hemistry in the oxidation of organics in the atmosphere has received less attention due, in part, to

180 bated deposition of anthropogenic N from the atmosphere has the potential to foster greater soil C st

181 stepwise, first under oxidizing and reducing atmospheres (imitating calcination and activation proces

182 loss of methane and other pollutants to the atmosphere, impacting climate and air quality.

183 starting mixtures representative of various atmosphere-impactor volatile combinations.

184 d 2.5 +/- 0.34 gigatons more carbon into the atmosphere in 2015, consisting of approximately even con

185 t the best packaging conditions were high-O2 atmosphere in combination with REO.

186 ssion from copper as well as the surrounding atmosphere in order to understand limitations of fs-fila

187 large amounts of carbon dioxide (CO2) to the atmosphere in response to increasing temperatures, repre

188 d an increase in the static stability of the atmosphere in the following break-to-active transition a

189 on accelerating rates of C exchange with the atmosphere in the most productive biome on earth.

190 ely to lead to greater emissions of V to the atmosphere in the near future.

191 (PMF) to identify the sources of PCBs to the atmosphere in this area and determine whether their conc

192 ve charge creates a region, known as the ion atmosphere, in which cation and anion concentrations are

193 ore, both oxides are unstable outside the O2 atmosphere, indicating the presence of active O atoms, c

194 Classic, model-based theory of land-atmosphere interactions across the Sahel promote positiv

195 redictability results from large-scale ocean-atmosphere interactions.

196 he importance of careful assessment of ocean-atmosphere internal variability in ENSO projections.

197 Pluto's atmosphere is cold and hazy.

198 Galactic escape velocity and whose peculiar atmosphere is dominated by intermediate-mass elements.

199 The history of Mars' atmosphere is important for understanding the geological

200 Isoprene oxidation in the atmosphere is initiated primarily by addition of hydroxy

201 e impact of this source on the summer Arctic atmosphere is likely to increase.

202 This likely indicates that HAT-P-26b's atmosphere is primordial and obtained its gaseous envelo

203 feedbacks on climate through changes in the atmosphere is sparse.

204 We conclude that Pluto's atmosphere is unique among Solar System planetary atmosp

205 ultraviolet irradiation it experiences, its atmosphere is unlikely to be substantially ablated over

206 sink and source of airborne particles to the atmosphere is unresolved.

207 l flux of water from the land surface to the atmosphere, is a major component of the hydrologic cycle

208 to be sustained by recently fixed C from the atmosphere (<60 years), despite stream DOC, CO2 , and CH

209 s nitrous oxide ([Formula: see text]) to the atmosphere mainly via microbially mediated denitrificati

210 Great Oxidation c. 2.4 Ga, the now oxidizing atmosphere masked that redox signal, but ancient soils r

211 Tree phenology mediates land-atmosphere mass and energy exchange and is a determinant

212 the surface heat flux from the oceans to the atmosphere may play an important role in creating region

213 including high levels of formic acid, in the atmosphere (measured by an online high-resolution time-o

214 also conducted a new transient coupled ocean-atmosphere model simulation across the YD that better re

215 Here, using fully coupled ocean-atmosphere model simulations, we show that accounting fo

216 easterly winds is coupled to a simple ocean-atmosphere model that is otherwise deterministic, linear

217 By using a dynamic soil-plant-atmosphere model, mortality risks associated with hydrau

218 are important both ecologically and to land-atmosphere models that couple terrestrial vegetation to

219 lcyclopropene (1-MCP) and dynamic controlled atmosphere monitored by respiratory quotient (DCA-RQ) wi

220 Fruit stored under dynamic controlled atmosphere monitored by respiratory quotient 1.3 (DCA-RQ

221 The dynamic controlled atmosphere monitored by respiratory quotient 1.5 (DCA-RQ

222 -the form ubiquitously present in the global atmosphere-occurs throughout the year, and that it is en

223 We demonstrate how recent atmosphere-ocean general circulation model (AOGCM) simul

224 We used output from four atmosphere-ocean general circulation models (AOGCMs; CCS

225 anomalies (1996-2005 and 2091-2100) from 29 Atmosphere-Ocean General Circulation Models implemented

226 omponents of internal variability in coupled atmosphere-ocean models are remarkably similar to the mo

227 These disruptions in the atmosphere, oceans, and across the terrestrial land surf

228 simulations that consider injection into the atmosphere of 15,000 Tg of soot, the amount estimated to

229 roduction of sulfur allotropes in the anoxic atmosphere of Archean Earth.

230 of aryl isocyanates from arylamines under an atmosphere of CO2 was developed.

231 lfur isotopes that took place in the Archean atmosphere of Earth.

232 he primary sources of opacity in the dayside atmosphere of KELT-9b are probably atomic metals.

233 Here we report the detection of TiO in the atmosphere of the hot-Jupiter planet WASP-19b.

234 Adding to the vibrant atmosphere of the meeting, a coalition of pancreatic can

235 os of up to approximately 10000 in the upper atmosphere of Titan; this observation likewise instigate

236 reacted with a dense steam or supercritical atmosphere of water and carbon dioxide that was outgasse

237 The atmospheres of orbiting Earth-sized planets are observat

238 re probably resembles the molecule-dominated atmospheres of other planets and, given the level of ult

239 gnatures of nitrogen, oxygen, and water rich atmospheres of terrestrial type exoplanets "highlighted"

240 mental sulfur aerosols are ubiquitous in the atmospheres of Venus, ancient Earth, and Mars.

241 gest reservoir of carbon exchanging with the atmosphere on glacial-interglacial timescales, the deep

242 Higher in the atmosphere, only the SF6-based estimate is available, an

243 shocks (stresses of up to one-third million atmospheres, or 33 gigapascals) to germanium, we report

244 small but persistent source of carbon to the atmosphere over 30 years after disturbance, while temper

245 In fine warm weather, the daytime convective atmosphere over land areas is full of small migrant inse

246 The presence of an atmosphere over sufficiently long timescales is widely p

247 rplay between the cryosphere, geosphere, and atmosphere over the last 30,000 y that led to extensive

248 PIST-1 system are capable of retaining their atmospheres over billion-year timescales.

249 modulated biospheric productivity and ocean-atmosphere oxygen levels over time.

250 Legs were chopped, modified atmosphere packaged (70%O2/30%CO2) and maintained under

251 ted the effect of REO combined with modified atmosphere packaging conditions (MAP), in our case, aero

252 eir importance in the monitoring of modified atmosphere packaging.

253 The atmosphere plays a fundamental role in the transport of

254 diation is retained at high altitudes in the atmosphere, possibly by absorbing chemical species such

255 capacity of 11.01 mmol g(-1) is achieved at atmosphere pressure by SIFSIX-1-Cu, and unprecedented lo

256 even at the temperature of its dayside, its atmosphere probably resembles the molecule-dominated atm

257 e density of nucleic acids and resulting ion atmosphere profoundly influence the conformational lands

258 Here we use a global array of ocean-atmosphere radiocarbon disequilibrium estimates to demon

259 ogen is isotopically heavier than the modern atmosphere, requiring a biologic cycle with nitrogen fix

260 and thermodynamic moistening of the warming atmosphere result in increased horizontal water vapor tr

261 cessary to form cirrus clouds in the Earth's atmosphere, routinely observed in polar regions, and typ

262 ical and biological processes, affecting the atmosphere, shallow lithosphere, hydrosphere, and biosph

263 relative humidity environment of the Martian atmosphere.Significant amounts of different perchlorate

264 fore and after two time points of controlled atmosphere storage.

265 tioning of semivolatile species found in the atmosphere, such as nitric acid, ammonia, and water.

266 m, and associated perturbations in the ocean-atmosphere system, likely had profound implications for

267 his study, we analyse whether a good working atmosphere that fosters mutual trust, support and a 'sen

268 ould be given to establishing a good working atmosphere that fosters mutual trust, support and a 'sen

269 s generated a large CO2 concentration in the atmosphere that has led to the so-called global warming.

270 In the absence of CO (under N2 atmosphere), the reaction did not proceed, and only star

271 In the lower solar atmosphere, the chromosphere is permeated by jets known

272 tics approach, it was assumed that in an air atmosphere, the primary compound in degradation pathways

273 Following injection into the atmosphere, the soot is heated by sunlight and lofted to

274 In an oxygen-containing atmosphere, these metals establish an atomically thin ox

275 Although generated by a rarefied atmosphere, they are paradoxically analogous to ripples

276 bducted sedimentary nitrogen (N) back to the atmosphere through arc volcanism has been advocated for

277 p roots connect deep soil/groundwater to the atmosphere, thus influencing the hydrologic cycle and cl

278 sistors as their environment is changed from atmosphere to high vacuum.

279 processes ranging from ice nucleation in the atmosphere to hydration of biomolecules and wetting of s

280 tent variable ocean heat is imprinted on the atmosphere to realize its predictive potential over land

281 ality and Morbidity in Heart Failure) or the ATMOSPHERE trial (Aliskiren Trial to Minimize Outcomes i

282 this gas ( approximately 42%) may reach the atmosphere via direct bubble transport (0-2 kt yr(-1)) a

283 f biological material from freshwater to the atmosphere via LSA is crucial for determining health and

284 eruption style and the evolution of Earth's atmosphere via planetary outgassing.

285 ence between the vapor pressures of leaf and atmosphere [VPD] increases).

286 and the relative proportion of C lost to the atmosphere vs. stored or transported downstream.

287 ted that the degradation process in an inert atmosphere was governed by decomposition reactions of es

288 life on planets not properly screened by an atmosphere was probably significant during the AGN phase

289 ia melanocarpa fresh fruits in argon and air atmospheres were investigated.

290 transfer of SOC from the mineral soil to the atmosphere when primary forests are logged and then unde

291 Our images show a nearly circular, dust-free atmosphere, which is very compact and only weakly affect

292 ng localized 'oxygen oases' under a reducing atmosphere, which left a characteristic oxidative weathe

293 r the best options for removing CO2 from the atmosphere while enhancing crop productivity of summer m

294 However, water exposed to the martian atmosphere will boil, and the sediment transport capacit

295 2+)), temperature (-35 to 25 degrees C), and atmosphere (with/without O2), making them a universal an

296 atter decay and carbon dioxide fluxes to the atmosphere, with phases of substantial soil carbon loss

297 oon Titan has a substantial nitrogen-methane atmosphere, with strong seasonal effects, including form

298 imetric decomposition of PE under controlled atmospheres, with NOx concentration relevant to industri

299 d carbon in the biosphere is returned to the atmosphere, yet there are limits to our ability to predi

300 y-BPI), which was readily oxidized in oxygen atmosphere yielding the corresponding disulfide analogue