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1 ort momentum and heat southward in the upper troposphere.
2 capacity, and can form new particles in the troposphere.
3 gnatures and photolytic rate constant in the troposphere.
4 ive scavenging of oxidized Hg from the upper troposphere.
5 e (O3) over the oceans and affect the global troposphere.
6 ms possess traits that allow survival in the troposphere.
7 nic material (SOM) are abundant in the lower troposphere.
8 uents of fine particulate matter (PM) in the troposphere.
9 tosphere and overestimate the warming of the troposphere.
10 sensing of water vapor and ice in the upper troposphere.
11 unidentified pathway to SOA formation in the troposphere.
12 al conditions from the polar to the tropical troposphere.
13 reveal missing Hg oxidation processes in the troposphere.
14 ay an important role in the chemistry of the troposphere.
15 e halogens for the oxidising capacity of the troposphere.
16 up to 80% of particles in the tropical free troposphere.
17 condary biogenic aerosol mass throughout the troposphere.
18 nomena such as stratospheric mixing into the troposphere.
19 llus pumilus, and Bacillus spp. in the upper troposphere.
20 one-dominated SO(2) oxidation pathway in the troposphere.
21 coupled chemistries of the stratosphere and troposphere.
22 ly resulting from subsidence of air into the troposphere.
23 RA-40 is unrealistic, particularly above the troposphere.
24 tanding the gas-phase chemistry of the lower troposphere.
25 ural and contrail cirrus clouds in the upper troposphere.
26 the dimer, should be detectable in the lower troposphere.
27 nly in the satellite data set with a warming troposphere.
28 s a result of greenhouse gas built-up in the troposphere.
29 -tropical planetary waves emanating from the troposphere.
30 vertical convection that perturbs the upper troposphere.
31 ility necessary to study NO2 anywhere in the troposphere.
32 amical coupling between the stratosphere and troposphere.
33 additional source of chlorine in the marine troposphere.
34 observed radical concentrations in the upper troposphere.
35 eflective methane condensation clouds in the troposphere.
36 rmation of ozone and other pollutants in the troposphere.
37 saturation over various regions in the lower troposphere.
38 and the degradation of methane in the Arctic troposphere.
39 l radicals as the driver of chemistry in the troposphere.
40 hen measurements had not been made above the troposphere.
41 nonitrates, drive NPF in the Amazonian upper troposphere.
42 y 2 degrees per degree of warming in the mid-troposphere.
43 whereas we did not observe production in the troposphere.
44 y driver of bioaerosol dynamics in the lower troposphere.
45 rowth of new particles in the tropical upper troposphere.
46 oposphere, but a negative trend in the upper troposphere.
47 the air maintain the oxidizing power of the troposphere.
48 lies that extend throughout the depth of the troposphere.
49 ing thermally to release NO(x) in the remote troposphere.
50 tially to the oxidized mercury burden in the troposphere.
51 tant particle source in the midlatitude free troposphere.
52 nt oxidant on global and local scales in the troposphere.
53 s of daytime HIO(3) in the remote lower free troposphere.
54 ajor loss channel for nitrogen oxides in the troposphere.
55 S-Chem with elevated ozone in the lower free troposphere.
56 ng in relatively weaker cooling in the upper troposphere.
57 ounts of gas and particulate matter into the troposphere.
58 burning smoke plumes during transport in the troposphere.
59 al variations over much of the remote marine troposphere.
60 of OH radicals upon alkene ozonolysis in the troposphere.
61 ter and hugely from radical reactions in the troposphere.
62 ce of OH sources and sinks across the remote troposphere.
63 om VOC oxidation can be kept relevant to the troposphere.
64 ury, particularly in the Arctic near-surface troposphere.
65 arable warming and moistening effects of the troposphere.
66 ying SO2 chemistry in the aerosol-containing troposphere.
67 ays with height, and disappears in the upper troposphere.
68 comprised the marine boundary layer and free troposphere.
69 ng aqueous secondary organic aerosols in the troposphere.
70 of the major types of aerosol present in the troposphere.
71 unds, ozone, and mercury in the Arctic lower troposphere.
72 e oxidative aging of organic aerosols in the troposphere.
73 from large-scale descent within the tropical troposphere.
74 s higher than predicted in the tropical free troposphere.
75 emissions and NOx at the surface and in the troposphere.
76 rce of the hydroperoxy radical (HO2 ) in the troposphere.
77 because of high water concentrations in the troposphere.
78 tion of ozone and PANs-type compounds in the troposphere.
79 ow clouds on the stratification of the lower troposphere.
80 x that exist in significant abundance in the troposphere.
81 to determine the lifetimes of MClDMS in the troposphere.
82 n in extensive regions of the tropical upper troposphere(1,2), resulting in tens of thousands of part
83 de (IO) in the tropical and subtropical free troposphere (10 degrees N to 40 degrees S), and show tha
86 tosphere(2,3) and warming the tropical upper troposphere(4-6), acting to strengthen the upper-level j
88 nce of microorganisms in the middle-to-upper troposphere (8-15 km altitude) and their role in aerosol
89 canic eruption (13 June 2011) from the upper troposphere (9 to 14 kilometers) into the lower stratosp
90 ction and loss pathways in the remote marine troposphere, according to box model simulations of OH co
91 by constraining wind and temperatures in the troposphere alone, even when the equatorial lower strato
92 pheric circulations(6-8) affecting the lower troposphere also occur, but the importance of their inte
94 ((.)OH) and chlorine ((.)Cl) radicals in the troposphere and by reference bacteria Methylorubrum exto
96 ally uniform temperature perturbation of the troposphere and Earth's surface that approximately follo
103 quantities of smoke aerosols into the upper troposphere and lower stratosphere (UT/LS), where they p
104 ese findings indicate that, at typical upper troposphere and lower stratosphere conditions, particles
105 d downward mixing from the midlatitude upper troposphere and lower stratosphere during PV intrusions.
107 maximize respectively in the tropical upper troposphere and near the surface over deserts, with both
108 ants such as sulfur dioxide (SO(2)) from the troposphere and power station flue gas is becoming more
109 O(3)-H(2)SO(4)-NH(3) nucleation in the upper troposphere and producing ice nucleating particles that
110 at even-MIF primarily originates in the free troposphere and propagates downward to surface air.
111 annel can impact the overall reaction in the troposphere and provide the spectroscopic information ne
113 ation and bidirectional coupling between the troposphere and stratosphere were dominant contributors
116 tive rates of temperature change between the troposphere and surface, and the mechanisms that produce
118 emonstrate the inherent coupling between the troposphere and the stratosphere and underscore the need
119 determine the radiative balance of the upper troposphere and the transport of water vapor across the
120 rosols that are transported downwards to the troposphere and travel around the globe with the general
122 ansport from Asia (air parcels from the free troposphere) and some high GOM dry deposition events wer
123 xport efficiency of BB emissions to the free troposphere, and chemical mechanisms of ozone production
124 ncentrations of OH and HO(2) radicals in the troposphere, and in particular the comparisons that have
125 influence the oxidizing capacity of Earth's troposphere, and iodine oxides form ultrafine aerosols,
126 (2)(*)) are also an important oxidant in the troposphere, and its gas-phase chemistry has been well s
127 cals are difficult species to measure in the troposphere, and we also review changes in detection met
128 nsport from the stratosphere or mid-latitude troposphere are inconsistent with our observations.
131 f less than 50 nanometres) in the lower free troposphere are transported from the free troposphere in
132 s recorded by thermometers) and in the lower troposphere (as monitored by satellites) diverge by up t
133 and lifetime, especially in the remote free troposphere, as well as the fate of carbon-containing re
136 nd in ozone at the surface and lower and mid-troposphere, but a negative trend in the upper troposphe
137 dical (OH) is the central oxidant in Earth's troposphere, but its temporal variability is poorly unde
138 o activate as depositional INPs in the upper troposphere by combining field measurements with laborat
139 arises because ultraviolet shielding of the troposphere by ozone becomes effective once oxygen level
140 suggest that additional OH formation in the troposphere can result from ozone interactions with the
142 osphere (caused by ozone) and warming of the troposphere (caused by well-mixed greenhouse gases).
143 , which penetrated into the equatorial upper troposphere, causing poleward shifts in the positions of
144 mazon basin, based on regular vertical lower-troposphere CH4 profiles covering the period 2010-2013.
146 timate is similar on a global average in the troposphere, contributes substantially to the D/H ratio
147 OS-Chem modeling results point toward a free troposphere contribution to mercury in wet deposition in
148 contrast, an initial finding that the lower troposphere cooled since 1979 could not be reproduced.
149 he concentration of water vapor in the upper troposphere could double by the end of the century as a
150 as a global-scale band in the tropical upper troposphere, covering about 40 per cent of Earth's surfa
151 stratosphere subsequently penetrate into the troposphere, demonstrating the importance of the dynamic
152 O(3) concentrations in the middle and upper troposphere, despite the fact that fossil-fuel burning r
153 gens influence the oxidative capacity of the troposphere directly as oxidants themselves and indirect
154 uld be a persistent organic pollutant in the troposphere due to its calculated half-life tau(1/2) of
156 rticles (pH 0-3) widespread across the lower troposphere enable acid-driven multiphase chemistry of I
162 ds when considering climate change-where the troposphere has been anomalously warming relative to the
163 n (NPF) from condensable vapours in the free troposphere has been suggested to contribute to CCN, esp
164 ion of the Northern Hemisphere extratropical troposphere has changed over recent decades, with marked
165 se-the boundary between the stratosphere and troposphere-has increased by several hundred meters sinc
166 the Northern Hemisphere, ozone levels in the troposphere have increased by 35 per cent over the past
167 ecadal-scale temperature change in the lower troposphere have indicated cooling relative to Earth's s
168 l organic peroxide in large abundance in the troposphere, highlights how photochemistry in the neglec
169 ols is a major loss channel for NO(x) in the troposphere; however, a quantitative understanding of th
170 aporation contributes significantly to lower troposphere humidity, with typically 20% and up to 50% o
171 nal Chemistry Experiment in the Arctic LOwer Troposphere (ICEALOT) cruise on the R/V Knorr in March a
172 cloud ice and, after sedimentation into the troposphere, impact cirrus clouds in the absence of othe
173 es, and efficiently transported to the upper troposphere in deep convective clouds, where it is mixed
174 e potential to also significantly impact the troposphere in mid- to late-winter and early spring.
176 nced transformation of TFA precursors in the troposphere in the summertime due to higher concentratio
178 at the surface and throughout the equatorial troposphere in the western/central Pacific paired with a
179 and descend through subsidence to the lower troposphere, in which they can serve as cloud condensati
180 direct photolysis processes occurring in the troposphere incorporating photochemical excitation and i
181 ept for ozone, satellite measurements of the troposphere indicate much smaller reductions, highlighti
184 ee troposphere are transported from the free troposphere into the boundary layer during precipitation
186 rticle formation (NPF) in the tropical upper troposphere is a globally important source of atmospheri
187 we find that this NPF in the tropical upper troposphere is a globally important source of CCN in the
188 New particle formation in the upper free troposphere is a major global source of cloud condensati
190 ng the formation of sulfate particles in the troposphere is critical because of their health effects
192 gaseous chlorine atom precursors within the troposphere is generally considered a coastal or marine
193 ly that the pattern of warming in the Arctic troposphere is highly unlikely to be as given in ERA-40
194 ganic compounds in combustion and in Earth's troposphere is mediated by reactive species formed by th
195 ocean; much of the air in the tropical upper troposphere is relatively depleted in HCN, and hence, br
198 long suggested that in the tropics, when the troposphere locally warms, the lower stratosphere locall
200 to the ozone variation in the tropical upper troposphere/lower stratosphere via the Ozone El-Nino Sou
201 -OOM production rates for the tropical upper troposphere, mainly resulting in nitrate IP-OOM but with
202 ds transported to this region from the lower troposphere may provide the source of HOx required to su
203 bate about changes in the temperature of the troposphere measured using the Microwave Sounding Unit (
206 depth, Terra Measurement of Pollution in the Troposphere (MOPITT) carbon monoxide (CO), Aqua Atmosphe
207 The prevailing view is that in the free troposphere, new particles are formed predominantly in c
208 traviolet radiation, altered stratosphere-to-troposphere O(3) flux, increased tropospheric hydroxyl r
209 supercluster, zonal convergence in the lower troposphere occurred between 500-1500 m levels above the
210 wn that when MJO wind anomalies in the lower troposphere of the eastern Pacific are westerly, Gulf of
213 luence the overall oxidizing capacity of the troposphere on a global scale by stimulating the product
214 ws their transport and mixing throughout the troposphere on a global scale, before they reach the str
215 reveal an enhancement of opacity in Titan's troposphere on the morning side of the leading hemispher
217 century increase of sulphate aerosols in the troposphere, or changes in the climate of the world's oc
218 nental boundary layers, as well as the upper troposphere over rainforests and Asian monsoon regions.
219 new particle formation in the tropical upper troposphere over the Amazon(1,2) and the Atlantic and Pa
221 affected by long-range transport in the free troposphere over the marine boundary layer into Nevada.
222 g-on period, a dominant warming in the upper troposphere over the tropics and on the surface at high
223 In the lowermost layer of the atmosphere-the troposphere-ozone is an important source of the hydroxyl
224 winds, convective storms, low-latitude upper troposphere, polar stratosphere, and northern aurora.
225 thicker elevated aerosol layer in the upper troposphere, potentially amplifying the severity of drou
226 ytic source of hydroxyl (OH) radicals in the troposphere, proceeds through energized Criegee intermed
228 le interactions of SOA in the free and upper troposphere, promote ice nucleation and facilitate long-
229 s mainly from the Pacific, the impact on the troposphere results from both the Pacific and Atlantic O
230 ll as the inferred temperatures in the lower troposphere, show only small warming trends of less than
233 vapor in the tropical and subtropical upper troposphere shows a wide range of isotopic depletion not
234 chemistry may be generally irrelevant to the troposphere, since its initial oxidant generation is sim
236 idation of volatile organic compounds in the troposphere; some models predict, and laboratory studies
237 ces, implying that even in the remote marine troposphere soot provided nuclei for heterogeneous sulfa
239 e in shaping the hemisphere-scale wintertime troposphere/stratosphere-coupled circulation and its var
240 sence of oxygenated organic compounds in the troposphere strongly influences key atmospheric processe
241 opogenic activities that add NO to the upper troposphere, such as biomass burning and aviation, will
242 factors and volcanic aerosols yields surface-troposphere temperature trend differences closest to tho
243 SST and to remote SST, represented by lower-troposphere temperature, are poorly captured in many mod
244 rth Atlantic sea surface temperature and mid-troposphere temperature; the latter is found to rise fas
249 of the brown carbon aerosol particles in the troposphere that absorb near-ultraviolet (UV) and visibl
250 mented major warming of the Antarctic winter troposphere that is larger than any previously identifie
251 50% of the global aerosol production in the troposphere, the chemical species and mechanism responsi
254 ddle and high latitudes can notably warm the troposphere there, thus reducing the equator-to-pole tem
255 nuously remove kinetic energy from the lower troposphere, thereby reducing the wind speed near hub he
256 circulation anomalies most likely affect the troposphere through changes to waves in the upper tropos
258 can also be subject to direct forcing by the troposphere, through quasi-steady, quasi-balanced dynami
259 stratospheric aerosol that they attribute to troposphere to stratosphere ascent via the Asian monsoon
260 ospheric circulation in the stratosphere and troposphere to the abundance of water vapor in the lower
261 individual tar balls transported in the free troposphere to the Climate Observatory "Ottavio Vittori"
266 imates is driven by enhanced stratosphere-to-troposphere transport of O3, and that reactive halogen c
267 cesses such as multi-annual variation of the troposphere, tropopause heightening, position and speed
268 ar, independent of the altitude (i.e., upper troposphere, tropopause region, and lowermost stratosphe
269 idering the abundance of isoprene SOA in the troposphere, understanding mechanisms of adverse health
270 al-column OH abundance throughout the remote troposphere (up to 70% of tropospheric mass) over the fi
271 n on the chemistry and dynamics of the upper troposphere (UT) based on direct aircraft observations o
272 tudes, minimum HCl values found in the upper troposphere (UT) were often near or below the detection
273 active iodine recycling on ice in the upper troposphere (UT), support the upper end of recent I(y) e
277 radicals OH and HO2 in the middle and upper troposphere were measured simultaneously with those of N
279 al that strong convection reaching the upper troposphere (where high atmospheric concentrations of so
280 in the relatively clean and cold upper free troposphere, where ammonia can be convected from the con
281 lobally important source of CCN in the lower troposphere, where CCN can affect cloud properties.
282 most abundant non-methane hydrocarbon in the troposphere, where it impacts ozone and reactive nitroge
283 t loss pathway of PF-2M3P and PF-3M2B in the troposphere whereas 2M3P is lost by both photolysis and
284 ical (OH), the most important oxidant in the troposphere, which accounts for approximately 90% of the
285 nd the warming trend in the equatorial upper troposphere, which appears to have sensitized MJO convec
286 lity in the TC outer region below the middle troposphere, which facilitates the local development of
287 phere is in striking contrast to the Earth's troposphere, which generally has a deeper low-stability
288 mperature and specific humidity in the lower troposphere, which in turn increases downward longwave r
289 sphere through changes to waves in the upper troposphere, which induce surface pressure changes that
290 ked cooling from the surface to lower-to-mid troposphere while resulting in relatively weaker cooling
292 mic and underappreciated aspect of the upper troposphere with potentially important impacts on the hy
293 elevated CO(2) levels, a region in the free troposphere with relatively constant CO(2) mole fraction
294 was monitored continuously over time in the troposphere with the use of aerosol time-of-flight mass
296 r of the temperature of the middle and upper troposphere, with a glacial cooling of -7.35 degrees +/-
297 re seen to rise from the middle to the upper troposphere within 30 minutes and dissipate within the n
298 ar Earth's surface that rises into the upper troposphere within mid-latitudes and accounts for up to
299 important because their presence in the free troposphere would facilitate transport over greater dist