ライフサイエンスコーパス: stratosphere

1 roposphere, tropopause region, and lowermost stratosphere).

2 l inorganic iodine (I(y)) is injected to the stratosphere.

3 its initial oxidant generation is similar to stratosphere.

4 ia, India, and Indonesia to enter the global stratosphere.

5 upwelling cannot be the main source for the stratosphere.

6 .5 h, in comparison with 3-5 days in Earth's stratosphere.

7 ction of sulfate aerosol precursors into the stratosphere.

8 late iodine (I(y,part)) from aircraft in the stratosphere.

9 the continued decrease of ozone in the lower stratosphere.

10 ne the penetration of the hot spots into the stratosphere.

11 easurements of infrared spectra of Jupiter's stratosphere.

12 latitudes in the upper troposphere and lower stratosphere.

13 ough to emit more than 5 Tg of soot into the stratosphere.

14 e crystals and more water vapor entering the stratosphere.

15 al range of chemical ozone loss in the lower stratosphere.

16 is transported from the troposphere into the stratosphere.

17 were observed in the 1999/2000 Arctic winter stratosphere.

18 significant potential to denitrify the lower stratosphere.

19 ne and chlorine compounds in the terrestrial stratosphere.

20 and possibly more humid future Arctic lower stratosphere.

21 the photochemical haze (or smog) in Titan's stratosphere.

22 e existence of unidentified NOX sinks in the stratosphere.

23 etecting eclipse-driven gravity waves in the stratosphere.

24 CO2 data is approximately 5 years in the mid-stratosphere.

25 m supersonic aircraft could reach the middle stratosphere.

26 significant injections of halogens into the stratosphere.

27 ing at 238 +/- 3 to 269 +/- 3 m s(-1) in the stratosphere.

28 )Cl suggesting a large contribution from the stratosphere.

29 causing strong ozone depletion in the lower stratosphere.

30 nsported from the distant troposphere or the stratosphere.

31 dine levels previously reported to reach the stratosphere.

32 ow a substantial moist bias in the lowermost stratosphere.

33 l increase the transport of mercury into the stratosphere.

34 nt to quickly loft CI material well into the stratosphere.

35 he abundance of water vapor in the lowermost stratosphere.

36 0 teragrams of water vapor directly into the stratosphere.

37 mportance of EPP on late winter/spring polar stratosphere.

38 lso contributes to depletion of ozone in the stratosphere.

39 ouds that can inject smoke directly into the stratosphere.

40 p to 70% of the ozone depletion in the lower stratosphere.

41 and the consequent depletion of ozone in the stratosphere.

42 d air rises, carrying the CI material to the stratosphere.

43 gh altitudes in the tropical entryway to the stratosphere.

44 f the injection of sulfate aerosols into the stratosphere.

45 surface is chemically processed in the lower stratosphere.

46 ern hemispheric aerosol burden in the middle stratosphere.

47 into aerosol particles that descend into the stratosphere.

48 not previously been considered to reach the stratosphere.

49 sions contribute to ozone destruction in the stratosphere.

50 trength of the meridional overturning of the stratosphere.

51 Hg (RM) forms throughout the troposphere and stratosphere.

52 iabatic overturning mass flux throughout the stratosphere.

53 he Atlantic and Tethysian realms through the stratosphere.

54 reactions characteristic of the present-day stratosphere.

55 serves as a major transport pathway into the stratosphere.

56 fy the total bromine loading injected to the stratosphere.

57 us chemical reactions in the troposphere and stratosphere.

58 in water vapour concentrations in the lower stratosphere.

59 are dynamically connected through the polar stratosphere.

60 posphere (9 to 14 kilometers) into the lower stratosphere.

61 may dominate the O(3) SC signal in the upper stratosphere.

62 osphere and between different regions of the stratosphere.

63 occurrence of processes native to planetary stratospheres.

64 tion characteristic of aerosols in planetary stratospheres.

65 ly navigating a superpressure balloon in the stratosphere(1) requires the integration of a multitude

66 tends to be larger (about 20%) in the lower stratosphere (12.5-17.5 km) and smaller (about 10%) with

67 Mountain waves also occurred throughout the stratosphere (15 to 45 kilometers) over a broad mountain

68 perature gradient by cooling the polar lower stratosphere(2,3) and warming the tropical upper troposp

69 trong westerly winds in the equatorial lower stratosphere (70 to 100 hPa) help to disrupt the WQBO by

70 frequently affected the Northern Hemisphere stratosphere aerosol loadings, whereas the Southern Hemi

71 Wave activity in the stratosphere also appears analogous to that occurring on

72 circulation strength at upper levels of the stratosphere amounts to at least 100 %.

73 reached 1.95 +/- 0.05(1sigma) in the middle stratosphere and 2.22 +/- 0.07 in the Arctic vortex vers

74 al stratosphere is the gateway to the global stratosphere and a commonly proposed location for solar

75 tely 50 kilometers, descend to the lowermost stratosphere and are followed by anomalous tropospheric

76 sotope slopes between the laboratory and the stratosphere and between different regions of the strato

77 ormed within the eastward phase in the lower stratosphere and cannot be accounted for by the standard

78 ects 5 Tg yr(-1) of sulphur dioxide into the stratosphere and cross-comparing simulations from 5 clim

79 anic eruption injecting material through the stratosphere and directly into the mesosphere.

80 oosted heterogeneous chemistry in the middle stratosphere and enhanced ozone production, compensating

81 nsidered against the background of a cooling stratosphere and geo-engineering plans to increase sulph

82 stent circulation anomalies in the lowermost stratosphere and is greatest during boreal winter.

83 d increase NO(x) concentrations in the polar stratosphere and mesosphere, causing reductions in extra

84 st particles (IDPs) collected in the Earth's stratosphere and meteorites are fragments of comets and

85 ey role in lofting pollutants from the lower stratosphere and nearly doubled the southern hemispheric

86 ne depletion and climate in the global lower stratosphere and offers predictions on future trends.

87 erestimate the observed cooling of the lower stratosphere and overestimate the warming of the troposp

88 s (1%) of the halogen inventory reaching the stratosphere and suggest that further constraints are ne

89 plored connection between the tropical upper stratosphere and the polar vortex.

90 recent cooling trend in the equatorial lower stratosphere and the warming trend in the equatorial upp

91 uary 2022 injected more water vapor into the stratosphere and to higher altitudes than ever observed

92 tivity of the atmospheric circulation in the stratosphere and troposphere to the abundance of water v

93 t of the tropopause-the boundary between the stratosphere and troposphere-has increased by several hu

94 sions through the coupled chemistries of the stratosphere and troposphere.

95 rtance of the dynamical coupling between the stratosphere and troposphere.

96 ent coupling between the troposphere and the stratosphere and underscore the need to assess not just

97 s the dynamics of the mid- and high-latitude stratosphere and weather in the lower atmosphere.

98 -12b lacks a prominent thermal inversion (or stratosphere) and has very efficient day-night energy ci

99 ery different isotopic fractionations in the stratosphere, and (ii) laboratory photolysis experiments

100 use substantial ozone depletion in the lower stratosphere, and any increases in future abundances (e.

101 ars, transporting more aged air to the lower stratosphere, and characterized by a larger relative con

102 etween 308 +/- 5 to 319 +/- 4 m s(-1) in the stratosphere, and gravity waves(7) propagating at 238 +/

103 torms, low-latitude upper troposphere, polar stratosphere, and northern aurora.

104 The object exploded in the stratosphere, and the ensuing shock wave blasted the cit

105 ard and westward wind jets in the equatorial stratosphere (approximately 16 to 50 kilometers altitude

106 g-to-core mass ratios of BC particles in the stratosphere are much greater than those in the free tro

107 onal variability of temperatures in Saturn's stratosphere as a manifestation of a wave phenomenon sim

108 ction of sulfur and halogen species into the stratosphere as a result of the Mt.

109 Our results show the stratosphere as a unique chemical environment where elem

110 erosol that they attribute to troposphere to stratosphere ascent via the Asian monsoon.

111 chemistry is irreversible transport from the stratosphere, associated with deep intrusions.

112 ssion, providing a detection of an exoplanet stratosphere at 5sigma confidence.

113 iation of the N2:O2 dimer produce NOx in the stratosphere at a rate comparable to the oxidation of N2

114 present throughout the upper troposphere and stratosphere at both poles.

115 its unexpected trajectory toward the middle stratosphere at ~35-kilometer altitude.

116 radionuclide, primarily created in the lower stratosphere, attaches to aerosols that are transported

117 rine and bromine will reach a maximum in the stratosphere between 1997 and 1999 and will decline ther

118 ols by the impact and their injection in the stratosphere, blocking incoming solar radiation.

119 l) is an important source of chlorine in the stratosphere, but detailed knowledge of the magnitude of

120 in tropical regions, mercury enters into the stratosphere, but the contribution of the stratosphere t

121 imentation of these large sizes in the lower stratosphere, but the nucleation process is not yet know

122 ome cases nitric acid) that are found in the stratosphere, but these are only effective for ozone dep

123 momentum from the ocean up to the tropo- and stratosphere by enhanced upward propagation of planetary

124 orange-brown smog, which is produced in the stratosphere by photochemical reactions following the di

125 /bromine free-radical chemistry of the lower stratosphere by shifting total available inorganic chlor

126 persistent ozone depletion is heating of the stratosphere by smoke, which strongly absorbs solar radi

127 burden of sulfate aerosols injected into the stratosphere by the eruption of Mount Pinatubo in 1991 c

128 n to forcing via wave-dissipation, the lower stratosphere can also be subject to direct forcing by th

129 e (O(3)), typically consumed by N(2)O in the stratosphere, can further accelerate N(2)O formation.

130 that cause denitrification in a nonvolcanic stratosphere cannot efficiently form in a volcanic envir

131 ary contributions are through cooling of the stratosphere (caused by ozone) and warming of the tropos

132 summer of 2019-2020 injected smoke into the stratosphere, causing strong ozone depletion in the lowe

133 ) (1997-1998)-induced changes in troposphere-stratosphere chemistry and dynamics.

134 se the significance of volcanic halogens for stratosphere chemistry and suggest that modelling of pas

135 In Titan's stratosphere, collisional stabilization of the initial C

136 that, at typical upper troposphere and lower stratosphere conditions, particles are formed by this nu

137 t tropospheric air enters the lower tropical stratosphere continuously, ascends, and is transported r

138 s, volcanogenic sulphate injections into the stratosphere cooled the NH preferentially, inducing a he

139 nt climate perturbation ends abruptly as the stratosphere cools and becomes supersaturated, causing r

140 tospheric temperature is confirmed-the lower stratosphere cools by approximately 2 degrees per degree

141 Our study suggests particle addition to the stratosphere could also perturb global radiative balance

142 Thus, hydration of the global stratosphere could be especially sensitive to changes of

143 It has been suggested that stratospheres could form in highly irradiated exoplanets

144 the hemisphere-scale wintertime troposphere/stratosphere-coupled circulation and its variability hav

145 ated parabolic reflector to be placed in the stratosphere directly above the ground station.

146 in decrease in the temperature of the Arctic stratosphere due to anthropogenic and/or natural effects

147 e driven by ozone depletion in the Antarctic stratosphere due to emissions of ozone-depleting substan

148 the midlatitude upper troposphere and lower stratosphere during PV intrusions.

149 c plume was injected directly into the lower stratosphere during the initial eruption well before rea

150 nd temperature that prevail in the Antarctic stratosphere during the period of maximum ozone (O3) dis

151 Air samples from the lower stratosphere exhibit 15N/14N and 18O/16O enrichment in n

152 The results show that the stratosphere facilitates the global dispersion of large

153 y, we analyze both the upper and lower polar stratosphere for links to extreme winter cold and snow i

154 luence the chemistry and the dynamics of the stratosphere for several years after the eruption.

155 AACP-origin hydration of the stratosphere has a poorly constrained role in ozone dest

156 arming relative to the zonal mean, the lower stratosphere has been anomalously cooling, and vice vers

157 The continuous injection of sulfur into the stratosphere has been suggested as a "geoengineering" sc

158 to the mean temperature trends in the lower stratosphere, highlighting the importance of the pattern

159 y ozone loss process in the cold polar lower stratosphere hinges on chlorine monoxide (ClO) and one o

160 y is well known for ozone destruction in the stratosphere, however reactive halogens also play an imp

161 methane into higher hydrocarbons in Titan's stratosphere implies a surface or subsurface methane res

162 rimarily due to the cooling within the upper stratosphere, implying a proportionate increase in clima

163 43% more volcanic sulfur is removed from the stratosphere in 2 months with the SO(2) heterogeneous ch

164 swift ozone depletion of 5% in the tropical stratosphere in just 1 week.

165 mponent that extends from the surface to the stratosphere in middle and high latitudes of both hemisp

166 ective injection into the mid-latitude lower stratosphere in summer.

167 at projected for a colder future nonvolcanic stratosphere in the 2010 decade.

168 ) hydrolysis can be important in the Earth's stratosphere, in the heterogeneous formation of sulfuric

169 In the stratosphere, IO radicals remain detectable (0.06 +/- 0.

170 When the flow in the equatorial upper stratosphere is also constrained, the timing and spatial

171 heric aerosol particles and confirm that the stratosphere is an important source of perchlorate, wher

172 Climate models predict that the lower stratosphere is cooling as a result of greenhouse gas bu

173 However, the impact of iodine in the stratosphere is highly uncertain due to the lack of prev

174 sphere alone, even when the equatorial lower stratosphere is in the correct phase of the quasi bienni

175 component that resides in the mesosphere and stratosphere is not of chondritic composition.

176 that the turbulent fraction of the tropical stratosphere is strongly modulated by the quasi-biennial

177 The tropical stratosphere is the gateway to the global stratosphere a

178 er vapor and CO entering the global tropical stratosphere is transported over the Asian monsoon/Tibet

179 val mechanisms are slow, so that much of the stratosphere is ultimately heated by the localized smoke

180 Saturn's south polar stratosphere is warmer than predicted from simple radiat

181 he QBO is in its easterly phase in the lower stratosphere, it favors stronger MJO activity during bor

182 ven if only 2% of these halogens reached the stratosphere, it would have resulted in strong global oz

183 meteorological phenomena in the winter polar stratosphere known as Sudden Stratospheric Warming (SSW)

184 ificant change in the chemistry of the lower stratosphere leading to a reduction potentially larger t

185 -lasting cold conditions in the Arctic lower stratosphere led to persistent enhancement in ozone-dest

186 ated with volcanic aerosols in the lowermost stratosphere (LMS) had not been considered.

187 hen the troposphere locally warms, the lower stratosphere locally cools.

188 of HCl with ozone found throughout the lower stratosphere (LS).

189 Pronounced cooling of the mid- to upper stratosphere, mainly driven by anthropogenic increases i

190 blished, water vapor injection deep into the stratosphere may exceed 7 tonnes per second.

191 oduces hot spots in its upper atmosphere and stratosphere near its poles, and the temperature maps de

192 Transport of air from the troposphere to the stratosphere occurs primarily in the tropics, associated

193 the organic aerosol formation regions in the stratosphere of a Saturn's moon Titan.

194 oling and ozone depletion in the polar lower stratosphere of both hemispheres, coupled with an increa

195 The smoggy stratosphere of Saturn's largest moon, Titan, veils its

196 reservoir, starting around 2007 in the lower stratosphere of the Northern Hemisphere, in contrast wit

197 d the largest volcanic sulfur release to the stratosphere of the past 7,000 y.

198 reported for the ratio of CH3D to CH4 in the stratosphere of the saturnian moon Titan.

199 ribute HOLW structures to transport from the stratosphere or mid-latitude troposphere are inconsisten

200 ed large volumes of sulphur dioxide into the stratosphere; or (3) MIF-S in rocks was mostly created b

201 In the upper stratosphere, our record extends back to 1986 and shows

202 In the lower stratosphere, our water vapour record extends back to 19

203 the substantial cooling of the global lower stratosphere over 1979-2003 occurred in two pronounced s

204 nt of risk associated with ozone loss in the stratosphere over the central United States in summer ba

205 ow more water vapor to travel into the lower stratosphere over the TP, effectively short-circuiting t

206 reported large ozone depletion in the lower stratosphere over the tropics.

207 er vapor convectively injected deep into the stratosphere over the United States can fundamentally ch

208 high resolution temperature structure in the stratosphere over the United States in summer that resol

209 of convective penetration of water into the stratosphere over the United States in summer using the

210 he globe and can penetrate and linger in the stratosphere over time scales of months.

211 York City, compounds that either deplete the stratosphere ozone or have significant global warming po

212 rease in the abundance of water vapor in the stratosphere (plausibly by as much as approximately 1 pa

213 the Asian monsoon/TP region enters the lower stratosphere primarily over the TP, and it is then trans

214 While ozone in the stratosphere protects the earth from harmful ultraviolet

215 tablished here that connects humidity in the stratosphere, relative humidity near the tropical tropop

216 A previous claim for the presence of a stratosphere remains open to question, owing to the chal

217 wavelength-dependent radiative effects, the stratosphere remains sufficiently cold and dry to hamper

218 partitioning of bromine and the input to the stratosphere remains uncertain.

219 Altogether, the stratosphere represents an important source of subseason

220 tion of calcite with acidic materials in the stratosphere results in a more complex aerosol than has

221 ll impact of the extra-tropical OWBCs on the stratosphere results mainly from the Pacific, the impact

222 the roles of the troposphere and equatorial stratosphere separately, using a split vortex event in J

223 The early stratosphere should have been dry, thereby precluding th

224 eric CO2 were observed to propagate into the stratosphere, showing that tropospheric air enters the l

225 The Earth's equatorial stratosphere shows oscillations in which the east-west w

226 Ozone loss is amplified in a denitrified stratosphere, so the effects of falling temperatures in

227 circulation changes initially induced in the stratosphere subsequently penetrate into the troposphere

228 Global mean lower stratosphere temperatures rose abruptly in January 2020

229 a plume of ice and water vapor in the lower stratosphere that occurs downwind of the ambient stratos

230 n Canadian wildfires injected smoke into the stratosphere that was detectable by satellites for more

231 by the meridional overturning of mass in the stratosphere, the Brewer-Dobson circulation.

232 In the stratosphere, the major source of O((1)D) is O(3) photol

233 Injecting sulfate aerosol into the stratosphere, the most frequently analyzed proposal for

234 o temperature changes in the troposphere and stratosphere, the relative importance of these two contr

235 , but are rapidly photolysed above the lower stratosphere, the timescale for their removal is set mai

236 In the lower stratosphere, these two estimates agree, and at a potent

237 Emanuel, Tropospheric thermal forcing of the stratosphere through quasi-balanced dynamics.

238 sociation of HOSO(2) occurs primarily in the stratosphere through the ejection of hydroxyl radicals (

239 s from increases in water vapor entering the stratosphere through the tropical tropopause layer, with

240 e theoretical deployment of particles in the stratosphere to enhance reflection of incoming solar rad

241 large amounts of CI material well within the stratosphere to enhance the aerosol loading, thereby inc

242 he stratosphere, but the contribution of the stratosphere to global mercury dispersion and deposition

243 oncentrations near the tropopause and in the stratosphere to increase outbound longwave radiation.

244 at there is a quasi-balanced response of the stratosphere to tropospheric heating [J.

245 etrated hundreds of kilometers into Saturn's stratosphere (to the 1-millibar region).

246 altered solar ultraviolet radiation, altered stratosphere-to-troposphere O(3) flux, increased troposp

247 erved in many UT air parcels, as a result of stratosphere-to-troposphere transport events.

248 The strength of stratosphere-to-troposphere transport is largely control

249 3/HOx in cold climates is driven by enhanced stratosphere-to-troposphere transport of O3, and that re

250 Stratosphere-troposphere exchange could be enhanced by t

251 ation, the strength of the polar vortex, and stratosphere-troposphere exchange make noticeable variab

252 ount of organic gases and particles into the stratosphere unprecedented in the satellite record since

253 reduction of ozone (up to 25%), cooling the stratosphere (up to 3 K) during late winter/spring.

254 temperature trends at the surface and in the stratosphere using large ensemble climate models followi

255 ere we study volcanic aerosol changes in the stratosphere using lidar measurements from the NASA CALI

256 through the Asian monsoon, and deep into the stratosphere, using satellite observations of hydrogen c

257 erosols into the upper troposphere and lower stratosphere (UT/LS), where they persist for months and

258 h transport from the upper troposphere/lower stratosphere (UT/LS).

259 e turbulent fraction of the equatorial lower stratosphere varies over a factor of ten depending on QB

260 tion in the tropical upper troposphere/lower stratosphere via the Ozone El-Nino Southern Oscillations

261 The observed smoke lifetime in the stratosphere was 40% shorter than calculated with a stan

262 At solar maximum, a warming of the summer stratosphere was found to strengthen easterly winds, whi

263 iennial oscillation (WQBO) in the equatorial stratosphere was unprecedentedly disrupted by westward f

264 mixing ratios of aerosol perchlorate in the stratosphere were 1 to 10 parts per trillion by mass (pp

265 ctional coupling between the troposphere and stratosphere were dominant contributors to variability.

266 ere on a global scale, before they reach the stratosphere where they release chlorine atoms that caus

267 tle slowly enough to be lifted high into the stratosphere, where degradation by ultraviolet radiation

268 es about half of the bromine that enters the stratosphere, where it plays an important role in ozone

269 the D/H ratio of H2 produced from CH4 in the stratosphere, where production is isolated from the infl

270 The smoke-laden air rises to the upper stratosphere, where removal mechanisms are slow, so that

271 o-noise characteristics of the mid- to upper stratosphere, where the signal of human-caused cooling i

272 to study the irreversible transport from the stratosphere, where the triple oxygen isotopes of CO2 ar

273 l chlorine and bromine, respectively, to the stratosphere, where they catalyze the destruction of ozo

274 omass-burning products into the mid-latitude stratosphere, where they destroy ozone, which protects u

275 Conversely, if there is a stratosphere-where temperature increases with altitude-t

276 have injected ~13 Tg of sulfur (S) into the stratosphere which produced various atmospheric optical

277 gases such as ozone and water vapour in the stratosphere - which affect surface climate - is influen

278 ions can loft ash, gases, and water into the stratosphere, which affects both human activities and th

279 gnificant quantities of SO4 aerosol into the stratosphere, which are known to affect ENSO strength by

280 se regulate the humidity of air entering the stratosphere, which in turn has a strong influence on th

281 ggested addition of calcite particles to the stratosphere, which one model suggests may enhance ozone

282 ozone loss and heating of the lower tropical stratosphere, which, in turn, would increase water vapor

283 The diurnal odd-nitrogen cycle in the stratosphere will be marked by a complex isotope signatu

284 nificant amounts of black carbon (BC) to the stratosphere with a residence time of several months.

285 se may typically allow entry of air into the stratosphere with as much as approximately 1.7 times the

286 organic aerosols in the "present-day" lower stratosphere, with similar impacts in both the North and

287 ude air is entrained into the tropical lower stratosphere within about 13.5 months; transport is fast

288 Moreover, the radiative heating of the lower stratosphere would be roughly 10-fold less than if that

289 ic eruptions, introducing particles into the stratosphere would reflect sunlight and reduce the level

290 Samalas reaching the stratosphere would result in catastrophic ozone depletio