Sudden stratospheric warming

A sudden stratospheric warming (SSW) is an event where the polar vortex of westerly winds in the winter hemisphere slows down or even reverses direction over the course of a few days. The change is accompanied by a rise of stratospheric temperature by several tens of kelvins.

History

The first continuous measurements of the stratosphere were taken by Richard Scherhag in 1951. He used radiosondes to take reliable temperature readings in the upper stratosphere (~40 km). It was his persistence which led him to witness the first ever observed stratospheric warming on 27 January 1952. After his discovery, Scherhag assembled a team of meteorologists specifically to study the stratosphere at the Free University of Berlin. This group continued to map the northern-hemisphere stratospheric temperature and geopotential height for many years using radiosondes and rocketsondes. In 1979 when the satellite era began, meteorological measurements became far more frequent. Although satellites were primarily used for the troposphere they also recorded data for the stratosphere. Today both satellites and stratospheric radiosondes are used to take measurements of the stratosphere.

Classification and description

Typically stratospheric meteorologists classify the vortex breakdown into three categories: major, minor, and final.

Sometimes a fourth category, the Canadian warming, is included because of its unique and distinguishing structure and evolution.

Major

These occur when the westerly winds at 60N and 10hPa (geopotential height) reverse, i.e. become easterly. A complete disruption of the polar vortex is observed and the vortex will either be split into daughter vortices, or displaced from its normal location over the pole.

According to the World Meteorological Organization's Commission for Atmospheric Sciences (Mclnturff, 1978): a stratospheric warming can be said to be major if at 10 mb or below the latitudinal mean temperature increases poleward from 60 degree latitude and an associated circulation reversal is observed (that is, the prevailing mean westerly winds poleward of 60 latitude are succeeded by mean easterlies in the same area).

Minor

Minor warmings are similar to major warmings however they are less dramatic, the westerly winds are slowed, however do not reverse. Therefore a breakdown of the vortex is never observed.

Mclnturff states: a stratospheric warming is called minor if a significant temperature increase is observed (that is, at least 25 degrees in a period of week or less) at any stratospheric level in any area of winter time hemisphere. The polar vortex is not broken down and the wind reversal from westerly to easterly is less extensive.

Final

The radiative cycle in the stratosphere means that during winter the mean flow is westerly and during summer it is easterly (westward). A final warming occurs on this transition, so that the polar vortex winds change direction for the warming, however do not change back until the following winter. This is because the stratosphere has entered the summer easterly phase. It is final because another warming cannot occur over the summer, so it is the final warming of the current winter.

Canadian

Canadian warmings occur in early winter in the stratosphere of the Northern Hemisphere, typically from mid November to early December. They have no counterpart in the southern hemisphere.

Dynamics

In a usual northern-hemisphere winter, several minor warming events occur, with a major event occurring roughly every two years. One reason for major stratospheric warmings to occur in the Northern hemisphere is because orography and land-sea temperature contrasts are responsible for the generation of long (wavenumber 1 or 2) Rossby waves in the troposphere. These waves travel upward to the stratosphere and are dissipated there, decelerating the winds and warming the Arctic. This is the reason that major warmings are only observed in the northern-hemisphere, with one exception. In 2002 a southern-hemisphere major warming was observed.[1] This event to date is not fully understood.

At an initial time a blocking-type circulation pattern establishes in the troposphere. This blocking pattern causes Rossby waves with zonal wavenumber 1 and/or 2 to grow to unusually large amplitudes. The growing wave propagates into the stratosphere and decelerates the mean zonal winds. Thus the polar night jet weakens and simultaneously becomes distorted by the growing planetary waves. Because the wave amplitude increases with decreasing density this easterly acceleration process is not effective at fairly high levels. If the waves are sufficiently strong the mean zonal flow may decelerate sufficiently so that the winter westerlies turn easterly. At this point planetary waves may no longer penetrate into the stratosphere [2]). Hence further upward transfer of energy is completely blocked and a very rapid easterly deceleration and the polar warming occur at this critical level, which must then move downward until eventually the warming and zonal wind reversal affect the entire polar stratosphere.

There exists a link between sudden stratospheric warmings and the quasi-biennial oscillation: If the QBO is in its easterly (westward) phase, the atmospheric waveguide is modified in such a way that upward-propagating Rossby waves are focused on the polar vortex, intensifying their interaction with the mean flow. Thus, there exists a statistically significant imbalance between the frequency of sudden stratospheric warmings if these events are grouped according to the QBO phase (easterly or westerly).

Weather effects

Although sudden stratospheric warmings are mainly forced by planetary scale waves which propagate up from the lower atmosphere, there is also a subsequent return effect of sudden stratospheric warmings on surface weather. Following a sudden stratospheric warming, the high altitude winds reverse to flow eastward instead of their usual westward. The eastward winds progress down through the atmosphere and weaken the jet stream, often giving easterly winds near the surface and resulting in dramatic reductions in temperature in Europe.

See also

References

  1. ↑ Manney, Gloria L.; Sabutis, Joseph L.; Allen, Douglas R.; Lahoz, William A.; Scaife, Adam A.; Randall, Cora E.; Pawson, Steven; Naujokat, Barbara; Swinbank, Richard (2005). "Simulations of Dynamics and Transport during the September 2002 Antarctic Major Warming". Journal of the Atmospheric Sciences. 62 (3): 690. Bibcode:2005JAtS...62..690M. doi:10.1175/JAS-3313.1.
  2. ↑ Charney, J. G.; Drazin, P. G. (1961). "Propagation of planetary-scale disturbances from the lower into the upper atmosphere". Journal of Geophysical Research. 66: 83. Bibcode:1961JGR....66...83C. doi:10.1029/JZ066i001p00083.

Further reading

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