Three Dimensional Propagation of Planetary Waves

Karoly, David J.; Hoskins, Brian J.

doi:10.2151/jmsj1965.60.1_109

Cited by 145 publications

(108 citation statements)

References 30 publications

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“…However, several studies of Rossby waves have shown that inclusion of the curvature terms, although entirely heuristic, can provide results that are in closer qualitative agreement with results obtained from more sophisticated models (e.g. Karoly and Hoskins, 1982;Hoskins and Ambrizzi, 1993). For this reason we include the curvature terms in our analysis, though it is important to emphasize that whether we include the curvature terms or not, our central results remain unchanged.…”

Section: Extended Charney-drazin Conditionsupporting

confidence: 55%

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Troposphere–stratosphere communication through local vertical waveguides

Nathan

Hodyss

2010

Quart J Royal Meteoro Soc

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The effects of zonally non-uniform background flow on the three-dimensional propagation of extratropical Rossby waves are examined using the WKB (Wentzel-Kramers-Brillouin) formalism. Emphasis is placed on the vertical propagation of wave activity. An extended Charney-Drazin (CD) condition that is valid for zonally non-uniform background flow is derived. The extended CD condition shows that local vertical propagation (trapping) is possible for wave scales for which the traditional CD condition predicts trapping (propagation). Local vertical propagation is shown to be strongly dependent on the phasing of the wave source relative to the background flow. Specifically, in zonally non-uniform background flow, vertical propagation is confined to local vertical waveguides whose formation is controlled by the orientation of the background wind relative to the wave fronts. Within the waveguide, vertical propagation is optimized when the disturbance wind field is parallel to the background potential vorticity gradient. As the wave packets move from the tropospheric source into the stratosphere they expand in zonal scale. The implications of these results to stratospheric sudden warmings are discussed.

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Section: Extended Charney-drazin Conditionsupporting

confidence: 55%

“…For this slowly varying background flow, we assume a phaseintegral (WKB: Wentzel-Kramers-Brillouin) solution for the disturbance field of the form (Karoly and Hoskins, 1982):…”

Section: Extended Charney-drazin Conditionmentioning

confidence: 99%

Troposphere–stratosphere communication through local vertical waveguides

Nathan

Hodyss

2010

Quart J Royal Meteoro Soc

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“…For a given zonal wave number and phase speed, l 2 indicates the mean flow ability to sustain the wave propagation, in particular the tendency to refract waves. As with the index of refraction, waves tend to refract towards larger values, and away from lower values of l 2 (Karoly and Hoskins, 1982).…”

Section: The Linear Qg Modelmentioning

confidence: 99%

The role of linear wave refraction in the transient eddy–mean flow response to tropical Pacific SST anomalies

Harnik

Seager

Naik

et al. 2010

Quart J Royal Meteoro Soc

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“…Considering the lag of model results in the mesosphere, the downward progression of the weak wind/reversal wind from the mesosphere to the stratosphere with each strong wave episode may be slower in reality than the model suggests. The weakening/reversal of the jet and the wave critical layer at progressively lower altitudes helps to alter the wave transmission condition at lower altitudes for more poleward propagation of the wave energy [Karoly and Hoskins, 1982], which is important for producing the major warming as discussed in the NCEP analysis.…”

Section: Time-gcm Analysismentioning

confidence: 99%

Dynamical coupling of the stratosphere and mesosphere in the 2002 Southern Hemisphere major stratospheric sudden warming

Liu

Roble

2005

Geophysical Research Letters

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NCEP data and a NCAR TIME‐GCM simulation are used to explore the dynamical coupling of the stratosphere and mesosphere during the 2002 Southern Hemisphere major stratospheric sudden warming. The analyses suggest the possibility of feedback interactions between the planetary wave forcing and the mesospheric/stratospheric mean state changes. Multiple strong planetary waves before the warming penetrate into the mesosphere and weaken the polar jet. They alter the wave transmission condition in favor of more upward‐poleward propagation of the wave energy at progressively lower altitudes. The jet reversal and the planetary wave surf zone also descend from the mesosphere down to the stratosphere, making wave breaking more likely at decreasing altitudes with each wave episode. These changes in the wave transmission and breaking conditions in the mesosphere and stratosphere may be critical for the extensive major stratospheric warming.

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Three Dimensional Propagation of Planetary Waves

Cited by 145 publications

References 30 publications

Troposphere–stratosphere communication through local vertical waveguides

Troposphere–stratosphere communication through local vertical waveguides

The role of linear wave refraction in the transient eddy–mean flow response to tropical Pacific SST anomalies

Dynamical coupling of the stratosphere and mesosphere in the 2002 Southern Hemisphere major stratospheric sudden warming

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