ライフサイエンスコーパス: tropospheric

1 , thus requiring a second source that may be tropospheric.

2 ng that processes controlling the background tropospheric abundance of nitrogen oxides are likely res

3 Compounds that readily absorb in the tropospheric actinic window (ionic organic complexes, PA

4 ganic compounds comprise a major fraction of tropospheric aerosol and understanding their chemical co

5 ghts relevant to the formation mechanisms of tropospheric aerosol building blocks.

6 The interactions of trace gases with tropospheric aerosol can have significant effects on bot

7 is shorter than that associated with either tropospheric aerosol loadings or previous characterizati

8 ory mass calibrations, IEPOX added > 0.4% to tropospheric aerosol mass in the remote tropics and up t

9 matter constitutes a significant fraction of tropospheric aerosol mass, and can influence CCN activit

10 ents of the concentration and composition of tropospheric aerosol particles capable of initiating ice

11 Tropospheric aerosols affect the radiative forcing of Ea

12 decrease of the global optical thickness of tropospheric aerosols by as much as 0.03 during the peri

13 e identified organosulfate compounds in free tropospheric aerosols by single particle mass spectromet

14 atial patterns indicative of the presence of tropospheric aerosols in the satellite-observed clear-sk

15 etween 5 and 19 kilometers reveal that upper tropospheric aerosols often contained more organic mater

16 into polyfunctional species widely found in tropospheric aerosols with light-absorbing brown carbon.

17 ropagate into the stratosphere, showing that tropospheric air enters the lower tropical stratosphere

18 ctuations in the collar and for upwelling of tropospheric air in late spring.

19 In the upper tropospheric air masses sampled, the production rate for

20 The range suggests that dehydration of upper tropospheric air occurs both by convective dehydration a

21 4 that shows GOM* and RM* levels in dry free tropospheric air of 198 +/- 57 and 229 +/- 58 pg m(-3) w

22 Tropospheric air pollution has impacts on scales ranging

23 ation between sea surface temperature, lower-tropospheric air temperature and total column water-vapo

24 recent deep convective outflow and aged free tropospheric air, suggesting a widespread abundance in t

25 ted upon the ERA-40 reanalysis, report polar tropospheric amplification of surface warming and attemp

26 On multidecadal time scales, tropospheric amplification of surface warming is a robus

27 (2-)) are among the most abundant species in tropospheric and stratospheric aerosols due to high leve

28 be responsible for the pronounced changes in tropospheric and stratospheric climate observed during t

29 is also important to the regulation of both tropospheric and stratospheric ozone.

30 n output and satellite-based measurements of tropospheric and stratospheric temperature change.

31 The spatial distribution of tropospheric and stratospheric temperature trends for 19

32 observed circulation changes and associated tropospheric and surface warming over northeastern Canad

33 formation of volatile oxidation products in tropospheric aqueous aerosols.

34 The tropospheric aqueous-phase aging of guaiacol (2-methoxyp

35 sustains autoignition and are implicated in tropospheric autoxidation that can form low-volatility,

36 Relevant to tropospheric biogeochemistry is irreversible transport f

37 table carbon isotope ratios to constrain the tropospheric budgets for the ozone-depleting halocarbons

38 try and climate models, since it impacts the tropospheric burden of sulfate aerosol, a major climate-

39 1, temperatures observed globally by the mid-tropospheric channel of the satellite-borne Microwave So

40 central reactants in many stratospheric and tropospheric chemical processes.

41 crease in noctilucent clouds, and changes in tropospheric chemistry and atmosphere-biosphere interact

42 tile organic compound emissions, and impacts tropospheric chemistry by influencing oxidants and aeros

43 Despite VOCs' critical role in tropospheric chemistry, studies for evaluating their atm

44 y reactions of interest in stratospheric and tropospheric chemistry.

45 ially powerful source of oxidants in aqueous tropospheric chemistry.

46 also suggest that a significant fraction of tropospheric chlorine atoms may arise directly from anth

47 emote locations across the globe reveal that tropospheric chlorine attributable to anthropogenic halo

48 resent evidence that recent trends in the SH tropospheric circulation can be interpreted as a bias to

49 Such a linkage is interpreted to be due to tropospheric circulation patterns in which positive PNA

50 ills and then swept over the SWTP by the mid-tropospheric circulation, rather than by upslope flow ov

51 aqueous secondary organic aerosol (aqSOA) in tropospheric cloud droplets and aqueous particles.

52 g Spectrometer reveal the presence of a vast tropospheric cloud on Titan at latitudes 51 degrees to 6

53 Tropospheric clouds form primarily in middle and high la

54 we report the presence of bright, transient, tropospheric clouds in tropical latitudes.

55 vial features and occasional rainstorms; and tropospheric clouds mainly (so far) in southern middle l

56 The recent discovery of midlatitude tropospheric clouds on Titan has caused much excitement

57 t in the formation and optical properties of tropospheric clouds over the ocean, a positive relations

58 been paid to low, high and vertically thick tropospheric clouds such as stratus, cirrus and deep con

59 y affect the "anomalous" oxygen signature in tropospheric CO(2) that should reflect the gross carbon

60 Industrial activities have caused tropospheric CO2 concentrations to increase over the las

61 Temporal variations in tropospheric CO2 were observed to propagate into the str

62 eoclimate applications of (17)O anomalies in tropospheric CO2, O2, mineral sulfates, and fossil bones

63 satellite Ozone Monitoring Instrument (OMI) tropospheric column NO2 densities.

64 ompound emitted to the atmosphere and shapes tropospheric composition and biogeochemistry through its

65 Here we characterize the tropospheric composition of oxygenated organic species,

66 iodine species of marine origin have on free tropospheric composition, chemistry, and climate.

67 n have hitherto shown no direct evidence for tropospheric condensation clouds, although there has bee

68 coefficient remains poorly determined under tropospheric conditions because of difficulties in makin

69 Master equation simulations conducted at tropospheric conditions identify that the collisionally

70 Numerical models reproduce the tropospheric conditions very well but have trouble expla

71 ticles was then measured under typical upper tropospheric conditions.

72 helium to model ozone-limited and ozone-rich tropospheric conditions.

73 redominates in the CH2OO decay under typical tropospheric conditions.

74 of diffuse glow and wave patterns forced by tropospheric convection.

75 Lead-210, a unique tracer of tropospheric deposition, also increased from 3200 Bq m(-

76 Stratospheric and tropospheric difluorodichloromethane (CF2Cl2) were found

77 The 2011 global mean tropospheric dry air mole fraction was 0.86 +/- 0.04 par

78 sition of tropospheric water vapour from the Tropospheric Emission Spectrometer (TES) aboard the Aura

79 loy recent space-based observations from the Tropospheric Emission Spectrometer with the GEOS-Chem at

80 Upper tropospheric equatorial westerly ducts over the Pacific

81 can be linked to a long-term trend in upper tropospheric equatorial westerly wind and subtropical je

82 cers of atmospheric deposition, we show that tropospheric fluxes of Hg and Pb are higher by a factor

83 rfacial oxidation, and the concentrations of tropospheric gases.

84 ydrogenases (e.g., Hyd2) to the oxidation of tropospheric H2 in soil ecosystems.

85 ontributes substantially to the D/H ratio of tropospheric H2.

86 nomycetes, serve as the main global sink for tropospheric H2.

87 acterized by large increases in mid-latitude tropospheric humidity and enhanced cycling of carbon thr

88 tionship between CAPE and a measure of lower-tropospheric humidity in simulations and in observations

89 Similar analyses of upper tropospheric humidity, cloud amount, surface air tempera

90 heric mixing ratios, we demonstrate that the tropospheric hydroxyl contribution from this source can

91 tosphere-to-troposphere O(3) flux, increased tropospheric hydroxyl radical concentration, and finally

92 ide with water can be an important source of tropospheric hydroxyl radicals.

93 for a distinction between stratospheric and tropospheric influences at remote East Antarctic sites.

94 analyses suggest that advection processes or tropospheric influences were unlikely to explain the str

95 crease of 0.8-34.8% of the overall inputs to tropospheric input.

96 ical circulation and a poleward shift of the tropospheric jet streams and their associated subtropica

97 atitudes, generating a poleward shift of the tropospheric jet, thereby relocating the main division b

98 eds back and reinforces the PJ pattern via a tropospheric Kelvin wave.

99 e influence of convective entrainment on the tropospheric lapse rate, and we demonstrate the importan

100 ermined for vinyl alcohol in the presence of tropospheric levels of (*)OH.

101 Its feasibility was demonstrated by making tropospheric measurements in flights aboard the Departme

102 tude and polar regions on the basis of these tropospheric measurements.

103 for this enrichment are condensation to form tropospheric methane clouds, fractionation occurring ove

104 However, much less is known about tropospheric mid-level clouds as these clouds are challe

105 gional changes in stratospheric volcanic and tropospheric mineral aerosols.

106 gued that in the tropics, the upper bound on tropospheric mixing and clouds is constrained by the rap

107 le in constraining the vertical structure of tropospheric mixing, tropopause temperature, and cloud-t

108 Tropospheric moist convection driven by elevated surface

109 ight a distinct radiative signature of upper tropospheric moistening over the period 1982 to 2004.

110 The tropospheric N2O concentrations have varied substantiall

111 te nitrate photolysis could be a substantial tropospheric nitrogen oxide source.

112 sources over the contiguous United States on tropospheric NO(x) and O(3) levels by using a global 3D

113 tion of ground-level NO2 concentrations from tropospheric NO2 columns retrieved from the Ozone Monito

114 C concentrations and satellite-retrieved CO, tropospheric NO2, and aerosol optical depth (AOD) (R(2)

115 ogen oxide (NO(x)) emissions, which increase tropospheric O(3) (warming) but also increase aerosols a

116 Tropospheric O(3) and sulfate both contribute to air pol

117 the exposure response of soybean to elevated tropospheric O(3) by measuring the agronomic, biochemica

118 ar-term warming by decreasing both CH(4) and tropospheric O(3).

119 ion, a small (approximately 20%) increase in tropospheric [O(3)] did not significantly alter photosyn

120 Tropospheric [O(3)] is predicted to reach a global mean

121 Most of the tropospheric O3 and methane (CH4) loss occurs at tropica

122 t as carbon sinks; prominent among these are tropospheric O3 and nutrient limitations(1,2).

123 ate response of oxidants, resulting in lower tropospheric O3 in cold climates while HOx (= OH + HO2 +

124 Increasing levels of tropospheric O3 in the Anthropocene may promote the form

125 The halogen-catalyzed loss of tropospheric O3 needs to be considered when estimating p

126 hane (CH4 ), an important greenhouse gas and tropospheric O3 precursor that has not yet been targeted

127 ught that temperature-dependent emissions of tropospheric O3 precursors and water vapour abundance de

128 to match NOx observations leads to elevated tropospheric O3.

129 ble for 34% of the column-integrated loss of tropospheric O3.

130 s and products expected in sea spray for low tropospheric [O3].

131 tion tail makes an important addition to the tropospheric OH budget.

132 ts the earth from harmful ultraviolet light, tropospheric or ground-level ozone is toxic and can dama

133 de emissions could increase the formation of tropospheric oxidants and secondary atmospheric aerosols

134 tures, with implications for the response of tropospheric oxidants and stratospheric thermal and mass

135 We find that tropospheric oxidants are sensitive to climate change wi

136 The response of tropospheric oxidants to climate change is poorly constr

137 The abundance of tropospheric oxidants, such as ozone (O3) and hydroxyl (

138 s"--carbonyl oxides--that play a key role in tropospheric oxidation models.

139 RO2) radicals are important intermediates in tropospheric oxidation of hydrocarbons, and their accura

140 Carbonyl oxide species play a key role in tropospheric oxidation of organic molecules and in low-t

141 intermediates," have long been implicated in tropospheric oxidation, there have been few direct measu

142 t atmospheric oxidant, capable of perturbing tropospheric oxidative cycles normally controlled by the

143 ors in calculations of global ozone budgets, tropospheric oxidizing capacity and methane oxidation ra

144 read and recurrent, and has implications for tropospheric oxidizing capacity, stratospheric compositi

145 e growing global background concentration of tropospheric ozone (O(3)), an air pollutant associated w

146 ations of elevated carbon dioxide (CO2 ) and tropospheric ozone (O3 ) for 11 years.

147 e global mean temperatures leading to higher tropospheric ozone (O3) concentrations in already pollut

148 ring atmospheric chemistry and causing sharp tropospheric ozone (O3) depletion in polar regions and s

149 Tropospheric ozone (O3) is potentially associated with c

150 Tropospheric ozone (O3) produces harmful effects to fore

151 Tropospheric ozone (O3), a global anthropogenic pollutan

152 modelling as NOx contributes to formation of tropospheric ozone (O3), a powerful air pollutant.

153 al cycling of nitrogen oxides (NOx) produces tropospheric ozone (O3), and NOx is traditionally consid

154 ibute to fine particulate matter (PM2.5) and tropospheric ozone air pollution, affecting human health

155 r terpenes, play a role in the production of tropospheric ozone and aerosols.

156 Tropospheric ozone and black carbon (BC) contribute to b

157 Tropospheric ozone and black carbon (BC), a component of

158 Two potent SLCPs, tropospheric ozone and black carbon, have direct effects

159 led that the short-term associations between tropospheric ozone and daily mortality rate were stronge

160 It is a precursor to tropospheric ozone and it influences the atmosphere's ox

161 stion sources of oxides of nitrogen altering tropospheric ozone and methane concentrations and enhanc

162 HONO, both of which play important roles in tropospheric ozone and OH production.

163 compounds (BVOCs) plays an important role in tropospheric ozone and secondary organic aerosol product

164 Tropospheric ozone and smoke aerosol measurements from t

165 High concentrations of tropospheric ozone are toxic, however, and have a detrim

166 e ozone refers to observed concentrations of tropospheric ozone at sites that have a negligible influ

167 s to peroxy acetyl nitrate (PAN), affect the tropospheric ozone budget, and in the remote marine envi

168 compounds, which is important for the global tropospheric ozone budget.

169 Much of the present tropospheric ozone burden is a consequence of anthropoge

170 A further reduction in the tropospheric ozone burden through bromine and iodine emi

171 New methods for retrieving tropospheric ozone column depth and absorbing aerosol (s

172 ut less appreciated is a concomitant rise in tropospheric ozone concentration ([O(3)]).

173 Results highlighted that tropospheric ozone concentration and air temperature pre

174 However, our analysis shows that tropospheric ozone concentration and subtropical intrusi

175 From 1979 to 1992 the tropospheric ozone concentration apparently increased by

176 cted to approximately double the global mean tropospheric ozone concentration, and further increases

177 udy has found a significant increase in free tropospheric ozone concentrations above the western USA

178 Mean 4-hour afternoon tropospheric ozone concentrations in Western Kenya incre

179 An estimate of tropospheric ozone concentrations was obtained from the

180 e local impacts of increased NO emissions on tropospheric ozone concentrations.

181 ern Hemisphere can account for this trend in tropospheric ozone concentrations.

182 Similar formation of bromine compounds and tropospheric ozone destruction may also occur at mid-lat

183 sted that the interannual variability of the tropospheric ozone distribution over the central-eastern

184 This increase in tropospheric ozone flux over the Pacific Ocean may affec

185 g marine aerosol formation and modification, tropospheric ozone formation and destruction, photooxida

186 irm and quantify the nonlinear dependence of tropospheric ozone formation on plume NO(x) (NO plus NO(

187 y, atmospheric heating from black carbon and tropospheric ozone has occurred at the mid-latitudes, ge

188 ing than the direct radiative forcing due to tropospheric ozone increases.

189 Tropospheric ozone is a serious air-pollutant, with larg

190 Tropospheric ozone is considered the most detrimental ai

191 Tropospheric ozone is known to damage plants, reducing p

192 Moreover, tropospheric ozone itself acts as an effective greenhous

193 Elevated tropospheric ozone leads to no reduction of forest produ

194 addition to reducing productivity, increased tropospheric ozone levels could alter terrestrial carbon

195 oir and play an important role in regulating tropospheric ozone levels in remote marine regions.

196 Increasing tropospheric ozone levels over the past 150 years have l

197 reenhouse gas and air quality by influencing tropospheric ozone levels.

198 A large proportion of tropospheric ozone loss occurs in the tropical marine bo

199 %) and accounts for up to 20% of the overall tropospheric ozone loss rate in the upper FT.

200 This study suggests that tropospheric ozone may not diminish forest carbon seques

201 However, tropospheric ozone pollution and climate change led to N

202 Epidemiologic studies have linked tropospheric ozone pollution and human mortality.

203 storage could be enhanced through minimizing tropospheric ozone pollution and improving nitrogen fert

204 cing per unit of emission due to aerosol and tropospheric ozone precursor emissions in a coupled comp

205 Methane is an important greenhouse gas and tropospheric ozone precursor.

206 hough many studies have linked elevations in tropospheric ozone to adverse health outcomes, the effec

207 TOMS instrument show El Nino signals but no tropospheric ozone trend in the 1980s.

208 int to multiple factors determining tropical tropospheric ozone variability.

209 urbation; the prediction of future trends in tropospheric ozone will require a full understanding of

210 cycles that catalytically destroy or produce tropospheric ozone, a greenhouse gas potentially toxic t

211 This study demonstrates that tropospheric ozone, although it damages plant metabolism

212 NO is a precursor to tropospheric ozone, an air pollutant and greenhouse gas.

213 ) maintained high concentrations of methane, tropospheric ozone, and nitrous oxide.

214 eeds further investigation, black carbon and tropospheric ozone, both of which are strongly influence

215 NO(x) emissions increase tropospheric ozone, but this increase and the resulting

216 Climate impacts of tropospheric ozone, fine aerosols, aerosol-cloud interac

217 onmental factors (climate, atmospheric CO2 , tropospheric ozone, nitrogen deposition, and land cover/

218 While El Nino leads to enhancements of upper tropospheric ozone, we find this influence does not reac

219 agents--including black carbon aerosols and tropospheric ozone--are noticeably better than greenhous

220 -phase, where they contribute to the loss of tropospheric ozone.

221 onments and implicated in the destruction of tropospheric ozone.

222 es, and therefore with abundant formation of tropospheric ozone.

223 t generate both urban photochemical smog and tropospheric ozone.

224 contribute significantly to organic mass in tropospheric particles.

225 gh studies that simulate a range of expected tropospheric particulate matter (PM) lifetimes, in order

226 eric particulate matter aid understanding of tropospheric photochemistry and are required for estimat

227 relative effects of atmospheric particles on tropospheric photochemistry, as well as possible inaccur

228 te observations of hydrogen cyanide (HCN), a tropospheric pollutant produced in biomass burning.

229 ) with NO represents one of the most crucial tropospheric processes, leading to terrestrial ozone for

230 iometric measurements were used to determine tropospheric profiles of the clear sky greenhouse effect

231 contrail cirrus clouds that can alter upper tropospheric radiation and water budgets, and therefore

232 icating that most anvil crystals form on mid-tropospheric rather than boundary-layer aerosols.

233 mate sensitivity, based on variations in mid-tropospheric relative humidity (RH) and their impact on

234 atmospheric moisture divergence and reduces tropospheric relative humidity in the tropics and subtro

235 bal dryness (suppressed rainfall and reduced tropospheric relative humidity) under CO2 warming from C

236 nships between tropical cyclone size and mid-tropospheric relative humidity.

237 Ozonolysis is a major tropospheric removal mechanism for unsaturated hydrocarb

238 Reaction with water may dominate tropospheric removal of Criegee intermediates and determ

239 As CFCs have no significant tropospheric removal process, but are rapidly photolysed

240 nd their reaction with (*)NO is an important tropospheric sink.

241 tion of sea-surface temperature patterns and tropospheric stability will be necessary for constrainin

242 is consistent with the effect of a change in tropospheric stability, as has recently been hypothesize

243 ing the troposphere and increasing the upper-tropospheric stability, the clustering of deep convectio

244 The tropospheric storm cell produced effects that penetrated

245 ons (forced by observed greenhouse gases and tropospheric sulfate aerosols) from the Geophysical Flui

246 ons forced with changes in greenhouse gases, tropospheric sulfate aerosols, and stratospheric ozone.

247 greater role of carbonyl oxides in models of tropospheric sulfate and nitrate chemistry than previous

248 n identifiable in 70% of the tests involving tropospheric temperature changes.

249 cies between model predictions and satellite tropospheric temperature data (and between the latter an

250 Trends in global lower tropospheric temperature derived from satellite observat

251 We have analyzed the global tropospheric temperature for 1978 to 2002 with the use o

252 this correction in the calculation of lower tropospheric temperature from satellite microwave measur

253 s in the initial analyses of satellite-based tropospheric temperature measurements.

254 sufficient magnitude to reconcile radiosonde tropospheric temperature trends and surface trends durin

255 ll remain large differences between observed tropospheric temperature trends and those simulated by a

256 tellite-based radiative emissions data yield tropospheric temperature trends that differ by 0.1 degre

257 hat stratospheric water vapor increases with tropospheric temperature, implying the existence of a st

258 ur satellite-derived version of middle/upper tropospheric temperature.

259 ndent radiosonde observations of surface and tropospheric temperatures confirm that, since 1979, ther

260 The resulting trend of reconstructed tropospheric temperatures from satellite data is physica

261 c and natural factors project an increase in tropospheric temperatures that is somewhat larger than t

262 At tropospheric temperatures, the ice surface is partially

263 it is in rapid thermal equilibrium at lower tropospheric temperatures.

264 tern of warming mode in near surface and low-tropospheric temperatures.

265 argued that the largest and most significant tropospheric trends can be traced to recent trends in th

266 tes with the satellite observations of NO(2) tropospheric vertical column densities (TVCDs) from four

267 ver an area of intensive surface mining, NO2 tropospheric vertical column densities (VCDs) are seen t

268 e traced to Northern Hemisphere and tropical tropospheric warming (cooling).

269 , both hemispheres have experienced enhanced tropospheric warming and stratospheric cooling in the 15

270 These measurements reveal multidecadal tropospheric warming and stratospheric cooling, punctuat

271 odels) cannot produce sustained global-scale tropospheric warming and stratospheric cooling.

272 ow us to unambiguously assign a cause to the tropospheric warming at this stage.

273 out of three recent satellite datasets, the tropospheric warming from 1979 to 2016 is unprecedented

274 t the most prominent annual mean surface and tropospheric warming in the Arctic since 1979 has occurr

275 For the tropics, the tropospheric warming is approximately 1.6 times the surf

276 rger than any previously identified regional tropospheric warming on Earth.

277 Tropospheric warming trends over recent 20-year periods

278 e cooling trend offsets the contributions of tropospheric warming.

279 the North Atlantic Oscillation or associated tropospheric warming.

280 Twenty-five percent of upper tropospheric water sampled is in ice particles whose iso

281 An all-HFCV fleet would hardly affect tropospheric water vapor concentrations.

282 here the interaction of convection with free tropospheric water vapor.

283 rus properties and the distribution of upper tropospheric water vapor.

284 ropical continents the isotopic signature of tropospheric water vapour differs significantly from tha

285 measurements of the isotopic composition of tropospheric water vapour from the Tropospheric Emission

286 tospheric processes, which in turn influence tropospheric weather and climate patterns on various spa

287 ric harbingers may be used as a predictor of tropospheric weather regimes.

288 t stratosphere and are followed by anomalous tropospheric weather regimes.

289 century, the CCMVal models predict that the tropospheric westerlies in Southern Hemisphere summer wi

290 In the past several decades, the tropospheric westerly winds in the Southern Hemisphere h

291 Decreases in lower-tropospheric winter westerlies across the region from 19