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

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

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

13 e atmosphere as Mount Bachelor received free tropospheric air masses on certain nights during the sam

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

15 4 that shows GOM* and RM* levels in dry free tropospheric air of 198 +/- 57 and 229 +/- 58 pg m(-3) w

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

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

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

19 orine isotope fractionation observed between tropospheric and bacterial degradation of CH(3)Cl provid

20 We test the hypothesis that this has reduced tropospheric and ground-level air pollution concentratio

21 (2-)) are among the most abundant species in tropospheric and stratospheric aerosols due to high leve

22 nHCs have a key role in regulating tropospheric and stratospheric ozone, while some hHNPs b

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

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

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

26 and range [Formula: see text], computed for tropospheric and stratospheric temperatures over 1979 to

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

28 formation of volatile oxidation products in tropospheric aqueous aerosols.

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

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

31 Relevant to tropospheric biogeochemistry is irreversible transport f

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

33 1, temperatures observed globally by the mid-tropospheric channel of the satellite-borne Microwave So

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

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

36 y reactions of interest in stratospheric and tropospheric chemistry.

37 ially powerful source of oxidants in aqueous tropospheric chemistry.

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

39 Regression of upper tropospheric circulation data on September sea-ice area

40 ean Western Boundary Currents (OWBCs) on the tropospheric circulation has recently been studied in de

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

42 t near-surface trends in Southern Hemisphere tropospheric circulation towards the end of the twentiet

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

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

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

46 Tropospheric clouds form primarily in middle and high la

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

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

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

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

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

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

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

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

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

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

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

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

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

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

61 redominates in the CH2OO decay under typical tropospheric conditions.

62 ticles was then measured under typical upper tropospheric conditions.

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

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

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

66 om BL to free atmosphere and increases lower tropospheric diabatic heating by shallow and congestus c

67 Stratospheric and tropospheric difluorodichloromethane (CF2Cl2) were found

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

69 e quasi-annular hemispheric structure in the tropospheric eddy-driven jetstreams and NAM variability.

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

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

72 Upper tropospheric equatorial westerly ducts over the Pacific

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

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

75 resulting Delta'(17)O values imply no direct tropospheric [Formula: see text] incorporation.

76 rfacial oxidation, and the concentrations of tropospheric gases.

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

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

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

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

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

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

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

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

85 ht into isoprene ozonolysis, which has broad tropospheric implications due to its critical role as a

86 The tropospheric implications of these reactions are evaluat

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

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

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

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

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

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

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

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

95 oughout the remote troposphere (up to 70% of tropospheric mass) over the first two ATom missions (Aug

96 Second, the uplift increases upper tropospheric mean easterlies and stratiform heating at t

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

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

99 gional changes in stratospheric volcanic and tropospheric mineral aerosols.

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

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

102 Tropospheric moist convection driven by elevated surface

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

104 The TROPOspheric Monitoring Instrument (TROPOMI) is used to

105 resent new measurements from the space-based TROPOspheric Monitoring Instrument (TROPOMI) launched in

106 part of wet season, using SIF data from the Tropospheric Monitoring Instrument (TROPOMI), which has

107 umn methane measurements from the spaceborne Tropospheric Monitoring Instrument (TROPOMI).

108 The tropospheric N2O concentrations have varied substantiall

109 and thereby affecting both stratospheric and tropospheric NAM-annularity.

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

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

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

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

114 stimate both the magnitude of tropical upper tropospheric NPF and the subsequent growth of new partic

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

116 ment (OMI) sensor enabled detection of lower tropospheric O(3) and its legitimacy has been validated.

117 ness of such satellite analyses on the lower tropospheric O(3) and its perturbations due to the precu

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

119 ls typically predict(4-7) an increase in the tropospheric O(3) burden of between 25 and 50 per cent s

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

121 y model simulations, to constrain changes in tropospheric O(3) concentrations.

122 ow its 1590-1958 AD mean, which implies that tropospheric O(3) increased by less than 40 per cent dur

123 cance for the OMI sensor to detect the lower tropospheric O(3) responses to the future emission reduc

124 also estimate that the radiative forcing of tropospheric O(3) since 1850 AD is probably less than +0

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

126 presence of abundant stratospheric and upper tropospheric O(3).

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

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

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

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

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

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

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

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

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

136 to match NOx observations leads to elevated tropospheric O3.

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

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

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

140 raphy (ATom) mission demonstrate that remote tropospheric OH is tightly coupled to the production and

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

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

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

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

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

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

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

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

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

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

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

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

153 ving simple CIs can significantly impact the tropospheric oxidizing capacity, enhance particulate for

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

155 Tropospheric ozone (O(3)) is a key component of air poll

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

157 l pollutants such as carbon dioxide (CO(2)), tropospheric ozone (O(3)), and particulate matter (PM) c

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

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

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

161 Tropospheric ozone (O3) is potentially associated with c

162 Tropospheric ozone (O3) produces harmful effects to fore

163 Tropospheric ozone (O3), a global anthropogenic pollutan

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

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

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

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

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

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

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

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

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

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

174 C globally by the simultaneous reduction of tropospheric ozone and methane.

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

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

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

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

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

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

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

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

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

184 Results highlighted that tropospheric ozone concentration and air temperature pre

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

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

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

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

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

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

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

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

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

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

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

196 Tropospheric ozone is considered the most detrimental ai

197 Tropospheric ozone is known to damage plants, reducing p

198 Moreover, tropospheric ozone itself acts as an effective greenhous

199 Elevated tropospheric ozone leads to no reduction of forest produ

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

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

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

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

204 %) and accounts for up to 20% of the overall tropospheric ozone loss rate in the upper FT.

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

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

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

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

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

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

211 w global supply chain relocates emissions of tropospheric ozone precursors and its impacts in shaping

212 The hydroxyl radical (OH) fuels tropospheric ozone production and governs the lifetime o

213 d isoprene emissions include higher rates of tropospheric ozone production, increases in the lifetime

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

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

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

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

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

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

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

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

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

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

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

225 ant atmospheric pollutants and precursors of tropospheric ozone, while the Middle East is a global em

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

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

228 onments and implicated in the destruction of tropospheric ozone.

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

230 ne radicals that facilitate the formation of tropospheric ozone.

231 contribute significantly to organic mass in tropospheric particles.

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

233 l (SOA) accounts for a large fraction of the tropospheric particulate matter.

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

235 ensor technologies (e.g., TROPOMI), study on tropospheric photochemistry will be rapidly advanced in

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

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

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

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

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

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

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

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

244 Potential lack of tropospheric relevance associated with these chemistries

245 Ozonolysis is a major tropospheric removal mechanism for unsaturated hydrocarb

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

247 and diverges deeper in the record revealing tropospheric signals for some previously assigned bipola

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

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

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

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

252 The tropospheric storm cell produced effects that penetrated

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

254 of the Ozone Monitoring Instrument (OMI) for tropospheric sulfur dioxide (SO(2)) and formaldehyde (HC

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

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

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

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

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

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

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

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

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

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

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

266 At tropospheric temperatures, the ice surface is partially

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

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

269 nstrument experiment to study the effects of tropospheric thunderstorms on the mesopause region and t

270 In particular, tropical upper-tropospheric troughs (TUTTs), as part of the summertime

271 ditions, OH is drastically reduced while non-tropospheric/undesired VOC reactants are not.

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

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

274 certainty [Formula: see text] is greater for tropospheric warming (8 to 15 y) than for stratospheric

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

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

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

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

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

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

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

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

283 low anthropogenic aerosol forcing, simulated tropospheric warming is larger than observed; detection

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

285 is larger than observed; detection times for tropospheric warming signals in satellite data are withi

286 Tropospheric warming trends over recent 20-year periods

287 For greenhouse-gas-driven tropospheric warming, larger noise and slower recovery f

288 the North Atlantic Oscillation or associated tropospheric warming.

289 e cooling trend offsets the contributions of tropospheric warming.

290 sently have a volatile cycle akin to Earth's tropospheric water cycle.

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

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

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

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

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

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

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

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

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

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