ライフサイエンスコーパス: atmospheric

1 time dilation is due to the increase in the atmospheric (14)C/(12)C ratio caused by the (14)C produc

2 vantages for the direct infusion analysis of atmospheric aerosol extracts.

3 surement gap related to our understanding of atmospheric aerosol impacts on climate and health.

4 uitous in the atmosphere and a source of new atmospheric aerosol particles of potentially global sign

5 tion (HESI) and nano-ESI for the analysis of atmospheric aerosol samples in the negative ionization m

6 dentities, properties, and concentrations of atmospheric aerosol surfactants in multiple environments

7 in the concentration and the composition of atmospheric aerosol, uncertainty exists as to whether th

8 hotosensitizer chemistry of HULIS in ambient atmospheric aerosols is unlikely to be a significant sou

9 ite (HMSi), which has not been identified in atmospheric aerosols, can emerge as the product of aqueo

10 umic-like substances (HULIS), extracted from atmospheric aerosols, retain the compositional complexit

11 cid, as a proxy for humic-like substances in atmospheric aerosols, to contribute to secondary organic

12 r, presumably associated with the passage of atmospheric African Easterly Waves.

13 diation and its underlying mechanisms during atmospheric aging have not been elucidated.

14 ations in many areas of chemistry, including atmospheric and environmental chemistry, biology, electr

15 understanding chemical dynamics relevant to atmospheric and geographical sciences.

16 n process in soot, which is important to its atmospheric and health effects.

17 ticularly the NAWH requires considering both atmospheric and oceanic mechanisms.

18 munity is advanced in investigating sources, atmospheric and oceanic transport, and forecasting clima

19 ine heatwave (2014-2016) associated with two atmospheric and oceanographic anomalies, the "Blob" and

20 Compared with previously-identified atmospheric and socioeconomic predictors, these slowly e

21 MSA can significantly alter the pH values of atmospheric aqueous aerosols and HMHSi is the most abund

22 These efforts are critical constraints to atmospheric assessment of anthropogenic fluxes in additi

23 nformer transition-state theory study of the atmospheric autoxidation in amines exemplified by the at

24 station measurements in Samoa combined with atmospheric back-trajectories provide novel information

25 the air temperature, significantly shallower atmospheric boundary layer, and weaker winds lead to sta

26 Atmospheric brown carbon (BrC) is an important contribut

27 h changes can have striking consequences for atmospheric C concentrations and the climate.

28 years, driven by increasing concentration of atmospheric carbon dioxide (CO(2)) and rising earth-surf

29 The oceanic uptake of atmospheric carbon dioxide (CO(2)) emitted by human acti

30 Elevated atmospheric carbon dioxide (eCO(2) ) is predicted to inc

31 stent with the expected net effect of rising atmospheric carbon dioxide and air temperature(7-9).

32 re, have a key role in the global balance of atmospheric carbon dioxide and oxygen.

33 bliquity (axial tilt)-can explain the lag of atmospheric carbon dioxide behind climate during glacial

34 g organic particles, which acts to lower the atmospheric carbon dioxide concentration.

35 -ecosystem warming and two years of elevated atmospheric carbon dioxide concentrations (eCO(2)).

36 wing the Stack process, the (14)C isotope of atmospheric carbon dioxide is fixed in the carbonate, an

37 on dioxide and thus contributed to the lower atmospheric carbon dioxide levels of the ice ages.

38 greenhouse gas emissions and capture excess atmospheric carbon dioxide(1,2).

39 sterly Wind-driven upwelling, each affecting atmospheric carbon dioxide.

40 and vegetated marine systems contributes to atmospheric carbon drawdown, but little empirical eviden

41 of Forest Transitions to the sequestering of atmospheric carbon will enable its potential to aid in c

42 Tropical forest responses to climate and atmospheric change are critical to the future of the glo

43 uence to test plant responses to climate and atmospheric change over the past 200 yr (including Pinus

44 We performed high-resolution (12 km x 12 km) atmospheric chemical transport modeling (WRF-Chem) for t

45 coupled Earth system model, with interactive atmospheric chemistry and a microphysical treatment of s

46 erse forest ecosystem in regional and global atmospheric chemistry and climate.

47 ed herein has considerable potential both in atmospheric chemistry and numerous others fields (e.g.,

48 que for gas-phase analysis in analytical and atmospheric chemistry mainly due to its very high mass r

49 should also be studied in relation to other atmospheric chemistry processes, such as facilitating mu

50 l chambers have been playing a vital role in atmospheric chemistry research for seven decades.

51 tion results from the EMAC (ECHAM5/MESSy for Atmospheric Chemistry) model were analyzed to assess the

52 utions is important in the context of, e.g., atmospheric chemistry, biophysics, and electrochemistry.

53 f these examples are taken from the field of atmospheric chemistry, they were selected because of the

54 nmental data on air monitoring and simulated atmospheric chemistry, we used a spatiotemporal model to

55 ries, and significantly impacts the regional atmospheric chemistry.

56 g isoprene ozonolysis continues to challenge atmospheric chemists.

57 While CH(3)Cl is the largest contributor of atmospheric chlorine, recent studies have shown that gro

58 the record is strongly influenced by AMV via atmospheric circulation anomalies.

59 Precipitation and atmospheric circulation are the coupled processes throug

60 y depends on distinct shifts in the regional atmospheric circulation associated with the existence of

61 This intensified energy flux reorganizes the atmospheric circulation leading to a northward shift of

62 eading mode of variability in North Atlantic atmospheric circulation) by an order of magnitude.

63 response by a shift in the dominant mode of atmospheric circulation, likely connected with a time-tr

64 Shallow atmospheric circulations(6-8) affecting the lower tropos

65 y (NBP) to climate change, and by changes in atmospheric circulations.

66 Possible explanations include mild wave or atmospheric climates and minimal anthropogenic impacts.

67 c incorporation of biomass-burning INPs into atmospheric cloud and climate models.

68 Rising atmospheric CO(2) (c(a)) is expected to promote tree gro

69 Elevated atmospheric CO(2) (eCO(2) ) generally increases carbon i

70 insic water use efficiency that track rising atmospheric CO(2) .

71 implicated as the drivers behind the rise in atmospheric CO(2) across the last deglaciation; however,

72 th Indian fingerprints on (early de-)glacial atmospheric CO(2) change.

73 Unravelling plant responses to rising atmospheric CO(2) concentration ([CO(2) ]) has largely f

74 The effects of cultivar and atmospheric CO(2) concentration ([CO(2) ]) on wheat-AMF

75 Abiotic factors, including atmospheric CO(2) concentration ([CO(2)]), can affect th

76 he combined effects of elevated salinity and atmospheric CO(2) concentration (c(a) ) on leaf gas exch

77 associated with periods of decreased global atmospheric CO(2) concentration during the LGM, confirmi

78 effects of nitrogen (N) addition and rising atmospheric CO(2) concentration on plant communities.

79 cribe how A responds to changes in light and atmospheric CO(2) concentration.

80 rrent ambient (440 ppm) and projected future atmospheric CO(2) concentrations (800 ppm).

81 The influence of terrestrial carbon flux on atmospheric CO(2) concentrations (DeltaCO(2) ) is estima

82 nt with Oi-1 was, thus, a response to coeval atmospheric CO(2) decline and continental-scale Antarcti

83 The ocean is a sink for ~25% of the atmospheric CO(2) emitted by human activities, an amount

84 Effects of atmospheric CO(2) fertilization, nitrogen deposition, cl

85 strial carbon sinks by increasing amounts of atmospheric CO(2) implies a weakening negative feedback

86 cean is thought to play an important role in atmospheric CO(2) increases associated with Pleistocene

87 tury and by 14%, 11% and 14% by 2091-2100 as atmospheric CO(2) increases.

88 Rising atmospheric CO(2) influences the terrestrial hydrologica

89 ale FFCO(2) emissions estimation through the atmospheric CO(2) inversion process.

90 ) is mainly shifted to the night period when atmospheric CO(2) is fixed by phosphoenolpyruvate carbox

91 Rising atmospheric CO(2) is intensifying climate change but it

92 e South Indian Ocean's capacity to influence atmospheric CO(2) levels and amplify the impacts of inte

93 Falling atmospheric CO(2) levels led to cooling through the Eoce

94 to terrestrial ecology, geochemical cycles, atmospheric CO(2) levels, and climate.

95 over the past ~285,000 years across varying atmospheric CO(2) levels, global ice volume and sea leve

96 ediated carbonate-silicate weathering cycle, atmospheric CO(2) partial pressure (pCO(2)) responds to

97 increasingly enriched with resources such as atmospheric CO(2) that limit ecosystem processes.

98 e we present a new high-resolution record of atmospheric CO(2) using the delta(11)B-pH proxy from 3.3

99 ise (SLR) and its interactions with elevated atmospheric CO(2), eutrophication, and plant community c

100 lytic reduction of carbon dioxide, including atmospheric CO(2), into methanol, under ambient conditio

101 ral in terms of an annual source or sink for atmospheric CO(2).

102 We found limited evidence of cultivar or atmospheric [CO(2) ] effects on plant-fixed carbon trans

103 e of terrestrial carbon uptake to increasing atmospheric [CO(2) ], that is the CO(2) fertilization ef

104 uptake via AMF was affected by cultivar and atmospheric [CO(2) ].

105 at in the future, despite predicted rises in atmospheric [CO(2) ].

106 maize (a) benefited less from an increase in atmospheric [CO(2) ]; (b) was less affected by higher te

107 Atmospheric cold fronts have an important influence on w

108 pase and lipoxygenase after the same time of atmospheric cold plasma (ACP) treatment were 77.50% and

109 The study indicates that atmospheric cold plasma can be tailored to mitigate the

110 hod does not allow the quantification of the atmospheric components accurately because the difference

111 thanogenic metabolisms strongly modifies the atmospheric composition, leading to a warmer but less re

112 The atmospheric concentration of several pollutants such as

113 ncubated for 21 h-showed about 15-fold lower atmospheric concentrations (3-4 pg.L(air)(-1)), while im

114 Atmospheric concentrations of 11 organophosphate esters

115 Understanding long-term trends in atmospheric concentrations of carbon dioxide (pCO(2)) ha

116 partitioning of VOC oxidation products under atmospheric conditions and thus greatly affect their atm

117 non-noble metal catalysts under solvent-free atmospheric conditions hinders their industrial applicat

118 ol particles and explore gel formation under atmospheric conditions in a contactless environment with

119 producibility, for instance, due to changing atmospheric conditions or sensitive positioning of the i

120 hurricane-force winds created sediment-laden atmospheric conditions, and that muddy rains rapidly set

121 stability without degradation under ambient atmospheric conditions.

122 ater repellency behavior well beyond typical atmospheric conditions.

123 derived SOA to nucleate ice under a range of atmospheric conditions.

124 or phenol and 47% yield for BCP-peroxy under atmospheric conditions.

125 mechanisms of monarch immunity under future atmospheric conditions.

126 roduced to the mass spectrometer to optimize atmospheric conditions.

127 Ammonium is an important atmospheric constituent that dictates many environmental

128 red for a full understanding of the planet's atmospheric convection and composition.

129 n acceleration in ice motion coincident with atmospheric cooling and a ~15% reduction in mean surface

130 Global carbon budgeting, atmospheric data, and forest inventories indicate a hist

131 s explored in relation to soil water supply, atmospheric demand and temperature.

132 w studies have focused on their abundance in atmospheric deposition in background environments.

133 Atmospheric deposition is an important source of nitroge

134 deposition to the watershed, or 184% of the atmospheric deposition to the embayments that discharge

135 urces, 51% of the septic sources, 98% of the atmospheric deposition to the watershed, or 184% of the

136 pollutants, reaching open waters mainly via atmospheric deposition.

137 We report the atmospheric discovery of a previously unquantified DMS o

138 We present a method for compensating the atmospheric dispersion of terahertz pulses using a cohor

139 oral variance in the Aleutian Low (a leading atmospheric driver of the PDO), and increasing correlati

140 hese results show that the photochemistry of atmospheric dust is both richer and more complex than pr

141 Ocean-atmospheric dynamical processes influence the wave chara

142 about 2.6 compared with the 2018 UK National Atmospheric Emissions Inventory.

143 ntrations and fate of NPAHs and OPAHs in the atmospheric environment are largely unknown.

144 o optimize the magnitude and distribution of atmospheric ethane and higher-alkane VOC emissions in th

145 anges over time without considering possible atmospheric feedbacks.

146 pted theory that culicine larvae respire via atmospheric gas exchange.

147 Atmospheric gravity waves generated by an eclipse were f

148 ong the sites suggests that OPEs with longer atmospheric half-lives and relatively high octanol-air p

149 g effects of a tropical storm followed by an atmospheric heatwave.

150 nce of these photodissociation mechanisms on atmospheric Hg chemistry, lifetime, and surface depositi

151 ation back to Hg(0) as a crucial step in the atmospheric Hg redox cycle.

152 s broadly considered as a possible source of atmospheric HONO in dark conditions, but the associated

153 bility driven largely by temporal changes in atmospheric humidity.

154 tial pathways for anoxygenic phototrophy and atmospheric hydrogen oxidation as supplemental energy so

155 how this system of interacting units in the atmospheric, hydrologic and geomorphological realm funct

156 tance was phenocopied in bacteria exposed to atmospheric hypoxia.

157 , hydrocarbon seepage is expected to have no atmospheric impact because the gas is typically consumed

158 e insoluble and soluble products of emerging atmospheric importance.

159 tribution of shale gas emissions to observed atmospheric increases in the global methane burden.

160 utes originates from various sources such as atmospheric inputs, rock dissolution and fertilizer resi

161 ropopause heightening, position and speed of atmospheric interface zones, as well as the poleward mov

162 e(1), potentially generating feedback on the atmospheric inventory of carbon dioxide.

163 ndamentally different approaches: "top-down" atmospheric inversions and "bottom-up" biosphere models.

164 Our set of atmospheric inversions and biosphere models, which were

165 ecause of the large spread in estimates from atmospheric inversions.

166 y, controlled experiments involving isolated atmospheric ions and neat saturated hydrocarbons in vacu

167 mpilation of global records of anthropogenic atmospheric lead (Pb) spanning the last 4000 years, an e

168 se ash particles are assumed to have a short atmospheric lifetime, and to not participate in sulfur c

169 Our finding shows that the atmospheric lifetimes of small OAs (e.g., FA) are highly

170 timates for 1,2-IHN Henry's law constant and atmospheric liquid water volume, we show that condensed-

171 time constant of about 6 h best explains our atmospheric measurements.

172 cing emission sources and transformations of atmospheric mercury with Hg stable isotopes depends on t

173 l be an important tool for future studies of atmospheric mercury.

174 Atmospheric methane (CH(4)) is a potent greenhouse gas,

175 n sources responsible for the sudden rise of atmospheric methane concentration (XCH(4)) since 2007, b

176 sidered to be the dominant natural source of atmospheric methane in terrestrial and shallow-water are

177 Satellite observations of atmospheric methane plumes offer a means for global mapp

178 orth Atlantic Oscillation (NAO) is the major atmospheric mode that controls winter European climate v

179 Using an atmospheric model forced with observed SSTs, we also fin

180 three-dimensional high-resolution idealized atmospheric model.

181 Using the NAME (Numerical Atmospheric Modeling Environment) particle dispersion mo

182 However, its inclusion in atmospheric models is hindered by a lack of understandin

183 An atmospheric moisture budget analysis shows that these en

184 In this regard, extraction of the ubiquitous atmospheric moisture is a powerful strategy allowing for

185 The ubiquity of atmospheric moisture offers an alternative.

186 re we present recently available data on the atmospheric mole fraction of CO(2), measured from six si

187 correlate with the proton affinities of the atmospheric molecules studied.

188 Here we show atmospheric monitoring station measurements in Samoa com

189 Our results imply that aerosol pH and atmospheric multiphase chemistry are strongly affected b

190 Atmospheric N deposition impacts ecosystem C storage, bu

191 inputs that have resulted from a tripling of atmospheric N deposition in the last century.

192 ts for emissions that might be sensed by the atmospheric network, but which are not included in inven

193 ain under conditions of chronically elevated atmospheric nitrogen (N) deposition.

194 Some plants fix atmospheric nitrogen by hosting symbiotic diazotrophic r

195 led the potential future impact of change in atmospheric nitrogen deposition on hypoxia in Chinese co

196 oxygen isotope compositions (Delta'(17)O) of atmospheric O(2) and [Formula: see text] are primarily r

197 Archean volcanic gases could have prevented atmospheric O(2) from accumulating until ~2.5 Ga with >=

198 variations of surface Earth temperature and atmospheric O(2) level.

199 including humans, thrive because of abundant atmospheric O(2), but for much of Earth history O(2) lev

200 standing carbon cycle dynamics observed from atmospheric observations and in using these observations

201 Instead, atmospheric observations show that emissions have increa

202 f atmospheric secondary organic aerosols and atmospheric OH recycling.

203 ld have been partly attributed to a range of atmospheric or landscape drivers, one often-forgotten dr

204 as used in this work to examine the roles of atmospheric organics in affecting ROS formation and anti

205 Because ozone is a common atmospheric oxidant, such compounds may be oxidized on c

206 When atmospheric oxidation is dominated by OH, OFR conditions

207 ement in urban areas, further increasing the atmospheric oxidizing capacity and facilitating secondar

208 uilibrium stromal oxygen concentration under atmospheric oxygen at 3 mW/cm(2) was 2.3% in 100 mum dec

209 t fracturing and erosion are as important as atmospheric oxygen in limiting pyrite reactivity over Ea

210 be rescued in vivo through brief exposure to atmospheric oxygen pressure.

211 into a ketone derivative in the presence of atmospheric oxygen.

212 g to speculation that such oxidation enabled atmospheric oxygenation.

213 transformation products were measured in 20 atmospheric particle samples collected in Chicago, in 21

214 ss burning is a significant global source of atmospheric particles and a highly variable and poorly u

215 exposed to elevated number concentrations of atmospheric particles are also exposed to more externall

216 Initial O-PTIR analysis of ambient atmospheric particles identified both inorganic and orga

217 Surface tension influences the fraction of atmospheric particles that become cloud droplets.

218 lar mechanism from ocean iodine emissions to atmospheric particles that is currently missing in model

219 l acidity largely regulates the chemistry of atmospheric particles, and resolving the drivers of aero

220 ical physiochemical properties of individual atmospheric particles.

221 miological studies address health effects of atmospheric particulate matter (PM) using mass-based mea

222 ers' reports, is created and used to analyze atmospheric phenomena responsible for floods.

223 Here, we described a cold atmospheric plasma (CAP)-mediated ICB therapy integrated

224 ith a special clamping device of non-thermal atmospheric plasma (NTAP) treatment using mixed gas for

225 n 300 daily PM(10) and further size-resolved atmospheric PM samples in the size range from 15 nm to 1

226 tent of global primary productivity and thus atmospheric pO(2) on geologic time scales.

227 clic aromatic hydrocarbons (PAHs) are common atmospheric pollutants and known to cause adverse health

228 ification from the standpoint of overlapping atmospheric pollution and social vulnerability.

229 transcriptional response induced by outdoor atmospheric pollution mixtures using field-based exposur

230 Atmospheric pollution represents a complex mixture of ai

231 verall, a reducing scenario leads to a lower atmospheric pressure at the surface and to a larger atmo

232 Atmospheric pressure chemical ionization (APCI) mass spe

233 Gas chromatography-atmospheric pressure chemical ionization-mass spectromet

234 HPLC coupled to tandem mass spectrometry by atmospheric pressure chemical ionization.

235 ost identical mass spectra as APCI involving atmospheric pressure conditions, the presence of many di

236 mass spectrometry data files generated by an atmospheric pressure gas chromatography-quadrupole time-

237 The mechanisms of these atmospheric pressure gas-phase reactions were explored t

238 ablation (LA) system to the liquid sampling-atmospheric pressure glow discharge (LS-APGD) microplasm

239 turated hydrocarbons at room temperature and atmospheric pressure has been performed in this system t

240 Atmospheric pressure ionization methods confer a number

241 Herein, we present a liquid atmospheric pressure matrix-assisted laser desorption/io

242 lectrospray ionization (ESI)(+), ESI(-), and atmospheric pressure photoionization (APPI)(+)) to chara

243 i)Pr(3))(2), Cp* = C(5)Me(5)) with ethene at atmospheric pressure produces the ethene-bridged diurani

244 tected at the surface during a period of low atmospheric pressure resulted from fractures of extremel

245 Atmospheric pressure sampling mass spectrometric methods

246 The atmospheric pressure that decreases with altitude affect

247 Reactivity measurements at atmospheric pressure with 30 mbar of methanol and CO (1:

248 of soil temperature, porewater salinity, and atmospheric pressure).

249 additional methods that ionize molecules at atmospheric pressure, (ii) ambient pressure ion mobility

250 tube ion mobility spectrometer, operated at atmospheric pressure, to a linear ion trap mass spectrom

251 lene but not propane at room temperature and atmospheric pressure, whereas the isostructural SIFSIX-3

252 temperature, and negatively correlated with atmospheric pressure, while the correlation pattern was

253 the outer surfaces of the cell electrodes at atmospheric pressure.

254 -port interface for subsequent ionization at atmospheric pressure.

255 tably, facile switching of the ion source to atmospheric-pressure chemical ionization with the exact

256 terization techniques to nanoparticles using atmospheric-pressure ion mobility-mass spectrometry (IM-

257 of LTP treatments against bacteria using an atmospheric-pressure plasma jet and show that LTP treatm

258 per, we present a new method to study global atmospheric processes and their changes during the last

259 Given future changes in climatic and atmospheric processes, climate and ecological dipoles ar

260 severe consequences for ecosystem function, atmospheric processes, sustainable resources and global

261 Atmospheric processing of alkenes, including isoprene, v

262 What atmospheric properties distinguish Jupiter from Saturn,

263 able if use can be made of past increases in atmospheric radiocarbon concentration or so-called Miyak

264 gs, which would affect the seasonal cycle of atmospheric radiocarbon concentrations recorded in diffe

265 A detailed computational study of the atmospheric reaction of the simplest Criegee intermediat

266 erature and precipitation extremes onto each atmospheric regime, we gain insight into the types of di

267 hese uncertainties, we use a global model of atmospheric Se cycling and a database of more than 600 s

268 However, estimates of global atmospheric Se fluxes are highly uncertain.

269 lts highlight the role of the ocean as a net atmospheric Se sink, with around 7 Gg yr(-1) of Se trans

270 OCs) in the bulk particle phase of a viscous atmospheric secondary organic aerosol (SOA) can have a p

271 nt implications for nucleation and growth of atmospheric secondary organic aerosols and atmospheric O

272 Experiments performed in an atmospheric simulation chamber suggest that the lifetime

273 olysis exerts a substantial control over the atmospheric SOA lifetime, with a likely dependence upon

274 ms are applicable to a broader extent across atmospheric species having carbonyl and hydroxyl functio

275 e bimolecular reaction of EHP with different atmospheric species.

276 ions of the plume width based on terrestrial atmospheric stability classes; a modified Gaussian dispe

277 Atmospheric sulfate aerosols have important impacts on a

278 region of New York, a historical hotspot for atmospheric sulfur and nitrogen deposition, features abu

279 Through alteration of wave-generating atmospheric systems, global climate changes play a funda

280 ndicates the influence of temperature-driven atmospheric teleconnections on wave-generation cycles.

281 talyst for societal shifts in MSEA via ocean-atmospheric teleconnections.

282 eric pressure at the surface and to a larger atmospheric thickness compared to an oxidised system.

283 Despite intense research, atmospheric transformations of isoprene leading to secon

284 environment, because of the overlap with the atmospheric transmission window.

285 ing, dissipating an object's heat through an atmospheric transparency window (8-13 mum) to outer spac

286 ization-selective thermal emission at the IR atmospheric transparency window for radiative cooling, i

287 e cooling lies in the high emissivity in the atmospheric transparency window through which heat can b

288 ric conditions and thus greatly affect their atmospheric transport and lifetime.

289 se state-of-the-art numerical simulations of atmospheric transport and meteorological data to follow

290 al vegetation models (DGVMs) coupled with an atmospheric transport model.

291 y be finely tuned to maximize fitness during atmospheric transport.

292 ve a greater potential to undergo long-range atmospheric transport.

293 ganophosphate esters (OPEs) were measured in atmospheric vapor and particle samples collected at six

294 om airborne remote sensing imagery indicates atmospheric venting from refinery hydrogen plants, landf

295 ssociated with similar amplifications in the atmospheric vertical and horizontal moisture advections.

296 Atmospheric warming threatens to accelerate the retreat

297 an appropriate sorbent is integrated in the atmospheric water generator.

298 Vegetation and atmospheric water vapor also had a profound influence on

299 e/(4)He lavas from Iceland (up to 42.9 times atmospheric) with anomalous (182)W and examine how Sr-Nd

300 -based detection and attribution analysis of atmospheric zonal wind, we show that the pause in circul