RAPID CYCLOGENESIS - METEOROLOGICAL PHYSICAL BACKGROUND

by KNMI and ZAMG


Rapid Cyclogenesis is accompanied by very distinct configurations in satellite images. In the literature the following four different types of development are often discussed within the same definition of Rapid Cyclogenesis:

However, within this manual and the satellite report, the conceptual model of the so-called Emerging Cloud Head is associated with Rapid Cyclogenesis and will therefore now be described in more detail.
While classical cyclogenesis through Wave development (see Wave ) is often slow and the Wave bulge dissolves after some time or produces a spiral after some days, Rapid Cyclogenesis usually leads to a fast development of a cloud spiral.

Within the polar front theory no separation between Wave development and Rapid Cyclogenesis can be found, and the distribution of the key parameters is very similar to, and even more distinct than, that for Wave development (see Key parameters). In addition to the Wave model, the jet streak and surrounding sinking dry air play key roles. The emerging cloud head in the initial stage usually appears in the left exit region of a jet streak. The jet streak is parallel to the initial cloud band with dry stratospheric air approaching downstream into the cloud head. This is seen as the typical black stripe in the WV imagery as well as the field of PV showing values higher than one PV units. While in the case of Wave development stratospheric air (if present at all) does not reach down to levels lower than 300 hPa, in the case of Rapid Cyclogenesis stratospheric air is a key feature and protrudes much further downward (down to approximately 500 hPa or even lower).

The dry sinking stratospheric air has a significant impact upon the cloud configuration. As it dissolves the cloudiness between the front and the cloud head, a spiral structure as well as the typical V - pattern develop. This is closely connected with special characteristics of relative streams.

There are several conveyor belts involved belonging to the different cloud systems. The cloudiness of the main frontal zone is produced by a typical Warm Conveyor Belt together with a humid relative stream from behind (see Cold Front ) while the dry stream from behind appears behind the poleward edge of the frontal cloud band. This is the dry stream containing stratospheric air described above. The cloud head is formed within the lower and mid-levels of the troposphere by a rapidly ascending conveyor belt advecting warm and moist air from lower latitudes beneath the Warm Conveyor Belt of the frontal zone. After crossing this Cold Front zone the conveyor belt often splits into a westward and an eastward flowing branch. This splitting of the relative flow leads to the convex-formed cloud edge at the pole ward side of the cloud head. This is comparable to the Occlusion process in Wave development (see Wave and Occlusion: Warm Conveyor Belt Type ).

As the advected air of the dry intrusion originates from the lower levels of the stratosphere, this flow is characterized by high values of potential vorticity. In the area where the dry intrusion is superimposed on the ascending conveyor belt from southern directions a potentially unstable stratification of the troposphere develops in which thunderstorms frequently occur (see Cloud structure in satellite images and Weather events).

As PV anomalies and baroclinic zones are involved Rapid Cyclogenesis may be a good example of the Hoskins theory. This theory states that an upper level PV anomaly, with its associated lowered tropopause, overrunning a low level baroclinic zone induces a cyclonic circulation within the upper levels of the troposphere. More information on this theory can be found in the introduction chapter "Parameters for the diagnosis of cloudiness - PV" (see Additional parameters and helpful tools for the diagnosis of cloudiness- Potential Vorticity ).
14 October 2002/06.00 UTC - Meteosat WV image; height of 2 units potential vorticity (in meters); magenta: potential vorticity
14 October 2002/12.00 UTC - Meteosat WV image; height of 2 units potential vorticity (in meters); magenta potential vorticity
14 October 2002/18.00 UTC - Meteosat WV image; height of 2 units potential vorticity (in meters); magenta potential vorticity
The three images above show the development of Rapid Cyclogenesis from a cloud head to a well-developed cloud spiral situated over the east Atlantic.
The image at 06.00 UTC (top left image) shows the initial stage of the development of a cloud head. The developing cloud head can be observed southwest of the British Isles. To its rear an intensive PV anomaly can be seen with high a gradient parallel to the frontal cloud band. The (dynamical) tropopause, here indicated with the height of 2 units PV, has lowered to a minimum of 6 km in the cold air to the rear of the frontal cloudband. During the next 12 hours this tropopause minimum, or PV - trough, representing stratospheric air approaches and overruns the developing cloud spiral of the Rapid Cyclogenesis.

Comparing again Wave development (see Wave ) and Rapid Cyclogenesis, a main difference can be found in the orientation of the relative stream forming the cloud head, or cloud bulge. It is similar to a Warm Conveyor Belt in the case of the Wave turning to east/north-eastern direction, but quite opposite in the case of Rapid Cyclogenesis turning to west/south-western directions. There are some differences between the two models, which can lead to this different behaviour:

  1. In the case of Rapid Cyclogenesis, two frontal zones (or at least a very broad one) exist which cause the rising conveyor belt to reach the rear side of the surface low. This may result, together with the upper stream, in a south-westward split.
  2. In the case of a Wave, the relative stream remains on the leading edge of the surface low, which may, together with the upper level stream, lead to a north-eastward split.

31 January 2002 12.00 UTC - Meteosat IR image; Magenta: height 1000 hPa, Cyan: height 500 hPa
12 December 2002 18.00 UTC - Meteosat IR image; Magenta: height 1000 hPa, Cyan: height 500 hPa
In the Rapid Cyclogenesis case of 31 January 2002 the upper level height contours have a straight west - east orientation while in the Wave case of 12 December 2002 the upper level height contours are, comparable to the surface pattern, also strongly curved.
31 January 2002/18.00 UTC - Vertical cross section; black: isentropes (ThetaE), red: temperature advection, orange: WV pixel values
31 January 2002/18.00 UTC - Meteosat WV image; magenta: relative streams 302K - system velocity: 262° 10 m/s, yellow: isobars 302K, magenta: relative streams, position of vertical cross section indicated
The isentropic surface of 302K represents the situation at upper levels as well as in the lower part of the troposphere.
Within, and in front of, the frontal zone the relative stream is rising towards the cloud head from below 700 hPa up to above 400 hPa. Behind the frontal zone and within the dark dry area a relative stream comes from areas with high PV values, representing stratospheric air descending to about 600 hPa in the dry intrusion.

SUB-MENU OF RAPID CYCLOGENESIS
CLOUD STRUCTURE IN SATELLITE IMAGES
KEY PARAMETERS