Multi‐Step Vertical Coupling During the January 2017 Sudden Stratospheric Warming

Becker, Erich; Гончаренко, Л. П.; Harvey, V. L.; Vadas, Sharon L.

doi:10.1029/2022ja030866

Cited by 23 publications

(26 citation statements)

References 95 publications

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“…In the present study, the large scales of the model are nudged to MERRA‐2 reanalysis in the troposphere and stratosphere, thereby allowing for the simulation of observed events. The GWs simulated by the nudged HIAMCM have been shown to agree with observations (Becker & Vadas, 2020; Becker et al., 2021, 2022). The current setup of the HIAMCM is for solar minimum conditions and the highest model layer is at z ∼ 400 km.…”

Section: Modelssupporting

confidence: 63%

Simulation Study of the 15 January 2022 Tonga Event: Development of Super Equatorial Plasma Bubbles

Huba

Becker

Vadas

2023

Geophysical Research Letters

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We present high‐resolution simulation results of the response of the ionosphere/plasmasphere system to the 15 January 2022 Tonga volcanic eruption. We use the coupled Sami3 is Also a Model of the Ionosphere ionosphere/plasmasphere model and the HIgh Altitude Mechanistic general Circulation Model whole atmosphere model with primary atmospheric gravity wave effects from the Model for gravity wavE SOurces, Ray trAcing and reConstruction model. We find that the Tonga eruption produced a “super” equatorial plasma bubble (EPB) extending ∼30° in longitude and up to 500 km in altitude with a density depletion of 3 orders of magnitude. We also found a “train” of EPBs developed and extended over the longitude range 150°–200° and that two EPBs reached altitudes over 4,000 km. The primary cause of this behavior is the significant modification of the zonal neutral wind caused by the atmospheric disturbance associated with the eruption, and the subsequent modification of the dynamo electric field.

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Section: Modelssupporting

confidence: 63%

Simulation Study of the 15 January 2022 Tonga Event: Development of Super Equatorial Plasma Bubbles

Huba

Becker

Vadas

2023

Geophysical Research Letters

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“…A simple ion drag parameterization is included as the only ionospheric process included in the model. Further details of the HIAMCM are given in Becker, Goncharenko, et al (2022) and and references therein.…”

Section: Model: Secondary Gws From Tongamentioning

confidence: 99%

Primary and Secondary Gravity Waves and Large‐Scale Wind Changes Generated by the Tonga Volcanic Eruption on 15 January 2022: Modeling and Comparison With ICON‐MIGHTI Winds

et al. 2023

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We simulate the primary and secondary atmospheric gravity waves (GWs) excited by the upward movement of air generated by the Hunga Tonga‐Hunga Ha'apai (hereafter “Tonga”) volcanic eruption on 15 January 2022. The Model for gravity wavE SOurce, Ray trAcing and reConstruction (MESORAC) is used to calculate the primary GWs and the local body forces/heatings generated where they dissipate. We add these forces/heatings to the HIgh Altitude Mechanistic general Circulation Model (HIAMCM) to determine the secondary GWs and large‐scale wind changes that result. We find that a wide range of medium to large‐scale secondary GWs with concentric ring structure are created having horizontal wind amplitudes of u′, v′ ∼ 100–200 m/s, ground‐based periods of τr ∼ 20 min to 7 hr, horizontal phase speeds of cH ∼ 100–600 m/s, and horizontal wavelengths of λH ∼ 400–7,500 km. The fastest secondary GWs with cH ∼ 500–600 m/s are large‐scale GWs with λH ∼ 3,000–7,500 km and τr ∼ 1.5–7 hr. They reach the antipode over Africa ∼9 hr after creation. Large‐scale temporally and spatially varying wind changes of ∼80–120 m/s are created where the secondary GWs dissipate. We analyze the Tonga waves measured by the Michelson Interferometer for Global High‐resolution Thermospheric Imaging (MIGHTI) on the National Aeronautics and Space Administration Ionospheric Connection Explorer (ICON), and find that the observed GWs were medium to large‐scale with cH ∼ 100–600 m/s and λH ∼ 800–7,500 km, in good agreement with the simulated secondary GWs. We also find good agreement between ICON‐MIGHTI and HIAMCM for the timing, amplitudes, locations, and wavelengths of the Tonga waves, provided we increase the GW amplitudes by ∼2 and sample them ∼30 min later than ICON.

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“…Oberheide (2022) also found a close relationship between the stratosphere polar vortex variability and the SW2 in ionosphere electron density, demonstrating that the influence of the stratosphere polar vortex variability on the SW2 in the MLT subsequently impacts the ionosphere. The strength of the stratosphere polar vortex has also been found to modulate gravity wave activity in the thermosphere and the associated traveling ionosphere disturbances (Becker et al., 2022; Frissell et al., 2016). Specifically, a strong stratosphere polar vortex was found to lead to an enhancement in TIDs while a weak stratosphere polar vortex decreased TID activity.…”

Section: Introductionmentioning

confidence: 99%

Influence of Stratosphere Polar Vortex Variability on the Mesosphere, Thermosphere, and Ionosphere

Pedatella

2023

JGR Space Physics

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During Northern Hemisphere winter, the stratosphere polar vortex that forms at high-latitudes in the Northern Hemisphere exhibits considerable variability. The stratosphere polar vortex variability is largely due to the presence, or absence, of planetary wave activity. During periods of strong planetary wave activity, the stratosphere polar vortex is weakened, leading to the occurrence of sudden stratosphere warming (SSW) events (Matsuno, 1971). Though identified based on changes in the stratosphere, SSWs have a wide range of impacts throughout the atmosphere (Baldwin et al., 2020;.In the mesosphere and lower thermosphere (MLT), SSW events are associated with changes in the circulation, mean winds, and atmospheric tides. At middle to high latitudes in the Northern Hemisphere, the zonal winds in the MLT reverse direction during SSWs (Hoffmann et al., 2007;Liu & Roble, 2002), which is primarily attributed to changes in gravity wave forcing (Limpasuvan et al., 2016;Liu & Roble, 2002;Zülicke et al., 2018). These zonal wind changes can extend across the equator into the Southern Hemisphere MLT through inter-hemispheric coupling (Körnich & Becker, 2010;Smith et al., 2020). The zonal mean zonal wind changes that occur during SSWs leads to enhancements in the migrating solar (SW2) and lunar (M2) semidiurnal tides (Chau et al., 2015;N. M. Pedatella et al., 2012;Zhang & Forbes, 2014). The SW2 is also enhanced due to changes in ozone forcing during SSWs (Siddiqui et al., 2019). Additional tidal variability occurs in non-migrating semidiurnal tides due to the non-linear interactions between the migrating tides and enhanced planetary wave activity (He et al., 2017;Liu et al., 2010;N. M. Pedatella & Liu, 2013). The changes in wave forcing during SSWs, including from gravity waves, planetary waves, and tides, alter the mean circulation of the MLT. During SSWs, the MLT circulation is characterized by enhanced clockwise and anti-clockwise circulation patterns in the Northern and Southern Hemispheres, respectively (

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Multi‐Step Vertical Coupling During the January 2017 Sudden Stratospheric Warming

Cited by 23 publications

References 95 publications

Simulation Study of the 15 January 2022 Tonga Event: Development of Super Equatorial Plasma Bubbles

Simulation Study of the 15 January 2022 Tonga Event: Development of Super Equatorial Plasma Bubbles

Primary and Secondary Gravity Waves and Large‐Scale Wind Changes Generated by the Tonga Volcanic Eruption on 15 January 2022: Modeling and Comparison With ICON‐MIGHTI Winds

Influence of Stratosphere Polar Vortex Variability on the Mesosphere, Thermosphere, and Ionosphere

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