On the dynamics of the spring seasonal transition in the two hemispheric
                        high-latitude stratosphere

Wang, Tongmei; Zhang, Qiong; Hannachi, Abdel; Lin, Yihua; Hirooka, Toshihiko

doi:10.1080/16000870.2019.1634949

Cited by 4 publications

(4 citation statements)

References 21 publications

(28 reference statements)

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“…Planetary wave activity from the troposphere to the stratosphere is on average stronger in austral spring compared to austral winter or boreal spring (Randel, 1988;Wang et al, 2019). Climatologically, in the SH late winter and spring the wave structure in the stratosphere is dominated by a quasi-stationary zonal wavenumber 1 (hereafter: wave-1) with contributions from a transient, eastward-moving zonal wavenumber 2 (hereafter: wave-2) (Randel, 1988;Mechoso et al, 1988;Manney et al, 1991;Harvey et al, 2002;Ialongo et al, 2012), which may contribute to zonal asymmetries in ozone depletion (Kravchenko et al, 2012).…”

Section: Introductionmentioning

confidence: 99%

The wave geometry of final stratospheric warming events

Butler

Domeisen

2021

Weather Clim. Dynam.

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Abstract. Every spring, the stratospheric polar vortex transitions from its westerly wintertime state to its easterly summertime state due to seasonal changes in incoming solar radiation, an event known as the “final stratospheric warming” (FSW). While FSWs tend to be less abrupt than reversals of the boreal polar vortex in midwinter, known as sudden stratospheric warming (SSW) events, their timing and characteristics can be significantly modulated by atmospheric planetary-scale waves. While SSWs are commonly classified according to their wave geometry, either by how the vortex evolves (whether the vortex displaces off the pole or splits into two vortices) or by the dominant wavenumber of the vortex just prior to the SSW (wave-1 vs. wave-2), little is known about the wave geometry of FSW events. We here show that FSW events for both hemispheres in most cases exhibit a clear wave geometry. Most FSWs can be classified into wave-1 or wave-2 events, but wave-3 also plays a significant role in both hemispheres. The timing and classification of the FSW are sensitive to which pressure level the FSW central date is defined, particularly in the Southern Hemisphere (SH) where trends in the FSW dates associated with ozone depletion and recovery are more evident at 50 than 10 hPa. However, regardless of which FSW definition is selected, we find the wave geometry of the FSW affects total column ozone anomalies in both hemispheres and tropospheric circulation over North America. In the Southern Hemisphere, the timing of the FSW is strongly linked to both total column ozone before the event and the tropospheric circulation after the event.

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Section: Introductionmentioning

confidence: 99%

The wave geometry of final stratospheric warming events

Butler

Domeisen

2021

Weather Clim. Dynam.

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“…Here, the SFWs are distinguished by the first occurrence of the wind reversal at 10 or 1 hPa (Hardiman et al., 2011; Thiélemont et al., 2019). Other classification methods, but less common, are by distinguishing between synchronous and asynchronous SFWs (Wang et al., 2019) or by the occurrence of Sudden Stratospheric Warmings (SSWs) in the preceding winter (Hu et al., 2015).…”

Section: Introductionmentioning

confidence: 99%

“…In the northern hemisphere there is a large interannual variability in the onset dates of the SFW varying by about 2 months between early March and late May (Butler et al., 2019; Savenkova et al., 2012; Wang et al., 2019; Waugh et al., 1999). The temporal‐vertical structure of the zonal wind reversal also varies from year to year where the wind reversal can first occur in the upper or middle stratosphere or even simultaneously at all altitudes in the stratosphere (Hardiman et al., 2011; Thiélemont et al., 2019).…”

Section: Introductionmentioning

confidence: 99%

Vertical Structure of the Arctic Spring Transition in the Middle Atmosphere

et al. 2021

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In the middle atmosphere (10-100 km) spring is the time period when the winter westerly winds reverse to summer easterly winds. The final breakdown and warming of the polar vortex is in general called "stratospheric final warming" (SFW). The timing and dynamical evolution of the stratospheric final warming is characterized by a combination of radiative forcing, due to seasonal changes of the solar zenith angle, and planetary wave (PW) forcing effects due to nonlinear interactions of PWs with the mean flow (Butler et al.

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“…This latter correlation is related to the predominant planetary wave number 2 activity, which can be recognized from the climatological circulation (vectors in Figure 10a). There is no such clear planetary wave activity at this level during the austral winter (Figure 10b) because the upward propagation of the planetary wave activity is prohibited by the strong zonal westerly wind (Charney and Drazin, 1961;Wang et al, 2019). This explains the lack This hemispheric difference is shown more clearly in the zonally averaged meridional cross-section of the correlation between the tropical lower-stratospheric water vapour and stratospheric temperature (shading, Figure 10c,d) and the zonal-mean zonal wind (contours, Figure 10c,d).…”

Section: 4mentioning

confidence: 99%

Tropical water vapour in the lower stratosphere and its relationship to tropical/extratropical dynamical processes in ERA5

Wang

Zhang

Hannachi

et al. 2020

Quart J Royal Meteoro Soc

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Stratospheric water vapour (SWV), in spite of its low concentration in the stratosphere as compared to the troposphere, contributes significantly to the surface energy budget and can have an influence on the surface climate. This study investigates the dynamical processes that determine SWV on interannual to decadal time-scales. First, we evaluate two SWV reanalysis products and show that SWV is better represented in a new-generation reanalysis product, ERA5, than in its predecessor, ERA-Interim. In particular, it is shown that SWV in ERA5 is highly consistent with observational data obtained from the SPARC Data Initiative Multi-Instrument Mean (SDI MIM). Second, we investigate the variability of tropical SWV and its relationship to dynamical stratospheric variables. The analyses show that the interannual variability in the tropical lower-stratospheric water vapour is closely linked to the tropical Quasi-Biennial Oscillation (QBO). When westerlies occupy the middle stratosphere and easterlies the lower stratosphere, a decrease is observed in lower-stratospheric water vapour due to a colder tropical tropopause and a QBO-induced enhanced residual circulation. On decadal time-scales, the composite analysis of the boreal winter in two typical periods shows that less SWV is related to a warm anomaly in the North Atlantic sea-surface temperature, which leads to stronger upward propagation of planetary wave activity at high latitudes, a weaker polar vortex and an enhanced residual circulation. The opposite occurs during periods with higher concentrations of SWV.

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On the dynamics of the spring seasonal transition in the two hemispheric high-latitude stratosphere

Abstract: View related articles View Crossmark data Citing articles: 1 View citing articles On the dynamics of the spring seasonal transition in the two hemispheric high-latitude stratosphere

Cited by 4 publications

References 21 publications

The wave geometry of final stratospheric warming events

The wave geometry of final stratospheric warming events

Vertical Structure of the Arctic Spring Transition in the Middle Atmosphere

Tropical water vapour in the lower stratosphere and its relationship to tropical/extratropical dynamical processes in ERA5

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