Extratropical cyclones View of an extratropical cyclone from above top panel and from the side bottom panel In top panel gray lines are isobars with pressures in mb red L indicates the center of the ID: 569274
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Slide1
SO254 Extratropical cyclones
View of an
extratropical
cyclone from above (top panel) and from the side (bottom panel). In top panel, gray lines are isobars with pressures in
mb
, red L indicates the center of the
extratropical
cyclone, colored arrows represent surface wind direction, magnitude, and temperature, blue shading indicates precipitation, and fronts are indicated by colored symbols. In the bottom panel, a vertical cross section is presented for the dashed pink line A to B in the top panel.
Source:
http://courses.knox.edu/envs150/overheads/topsidecyclone.JPG
Slide2
What is an extratropical cyclone?
An extratropical cyclone (ETC) is an area of low pressure, often migratory and with frontal boundaries, typical of the middle and high latitude regions of the world
ETCs develop as part of
cyclogenesis
:
During
cyclogenesis
, vorticity (spin) of low-level air increases, updrafts increase near the center, and surface pressure decreases
The life cycle of an
extratropical
cyclone typically lasts 4-8 days
Key processes that
favor
cyclogenesis
include: divergence aloft, surface air convergence, advection of cyclonic vorticity aloft, warm- and cold-air advection near the surface
Key processes that disrupt
cyclogenesis
include: surface friction, convergence aloft, advection of
anticyclonic
vorticity aloftSlide3
Life cycle of an ETC: Step 1
This stage is called the “spin up” stage
Surface front (stationary), clouds (gray shaded), temperatures (dashed lines) and isobars (solid black lines, in
kiloPascals
)
Upper-level jet stream (dashed arrow) and region of upper-level divergence (labeled “D”)
First step:
Region of upper-level divergence and/or upper-level vorticity advection moves overhead of a surface temperature gradient
Consequence of first step:
Air rises in the area beneath the divergence and/or the vorticity advection
Rising air
stretches
the air column, causing it to rotate
Surface convergenceSlide4
Life cycle of an ETC: Step 2
(First step still remains in place)Region of upper-level divergence and/or upper-level vorticity advection remains overhead of a surface temperature gradientSecond step:
Fronts develop. A warm front develops at the leading edge of the warm air moving north to the east of the ETC. A cold front develops at the leading edge of the cold air moving southeast to the west of the ETC.
Consequence of second step:
The wavelength of the upper-level jet trough and jet stream shortens. Divergence aloft and positive vorticity advection aloft both increase.
This stage is called the “frontal wave” stage
During “frontal wave” stage: a “wave” of low pressure develops along a stationary temperature gradient, in response to forcing from aloftSlide5
Life cycle of an ETC: Step 3
(First two steps still remain in place)Region of upper-level divergence and/or upper-level vorticity advection remains overhead of a surface temperature gradientWarm- and cold-air advection continue occurring in the lower atmosphere, acting to build a ridge ahead of the ETC and a trough behind it. Surface fronts are also becoming well defined
Third step:
Surface air pressures fall (sometimes quickly), at the core center of the ETC. Precipitation, sometimes heavy, develops along the frontal boundaries. Upper-level divergence and vorticity advection are maximized.
Consequence of third step:
Falling surface pressures promote intensification of surface temperature gradients, a process called
frontogenesis
This stage is called the “deepening” stage
During “deepening” stage: Air circulation around developing low pressure moves warm air north and cold air south, transforming stationary frontal boundary into a warm front and a cold frontSlide6
Life cycle of an ETC: Step 4
(First three steps still remain in place)Region of upper-level divergence and/or upper-level vorticity advection remains overhead of a surface temperature gradientWarm- and cold-air advection continue occurring in the lower atmosphere, acting to build a ridge ahead of the ETC and a trough behind it. Surface fronts are also becoming well defined
Surface pressures fall in the center of the low
Fourth step:
Precipitation and latent heat release promote quick deepening of surface low pressure. Cold air advances faster south and east than warm air advances north and west. Surface winds are maximized, upper-level trough is deepest, divergence aloft and vorticity advection aloft are strongest
Consequence of fourth step:
Surface pressures are lowest, precipitation rates greatest, winds strongest
This stage is called the “mature” stage
During “mature” stage: Lowest central pressure of the ETC, greatest surface wind speeds, heaviest precipitation, most intense fronts (most intense temperature gradients)Slide7
Life cycle of an ETC: Step 5
Fifth step: Cold front overtakes warm frontConsequences of fifth step:Surface temperature gradient weakens and shifts east of the ETC
Cold-air advection located east of the ETC causes upper-level trough to move east, with axis of upper-level trough now east of surface low
Upper-level convergence and
anticyclonic
vorticity advection are now present overhead of the surface low
Both promote sinking air in the column over the surface low
Cyclolysis
(weakening) occurs, until eventual dissipation of the ETC
This stage is called the “decay” stage
During “decay” stages: Cold front overtakes warm front, shifts greatest temperature gradients east of ETC center. Cold-air advection shifts east, helping upper-level trough to move east, and replacing upper-level divergence/cyclonic vorticity advection with upper-level
convergence
and anticyclonic vorticity advection over the surface low.Slide8
Evolution of frontal boundaries during ETC life cycle
Frontal wave (a)Stationary front still (little circulation around surface low)Mature cyclone (b)
Strong winds around surface low
Cold front nearly overtakes warm front
Decay (c)
Cold front overtakes warm front
Surface low pressure separated from strong temperature gradientsSlide9
Another view of ETC development
View from top: surface low located to the east of trough axis, ideally beneath area of greatest divergence aloft and area of maximum cyclonic vorticity advectionIt’s possible, in the real atmosphere, that the area of greatest divergence aloft doesn’t align with the area of maximum cyclonic vorticity advection
“Warm air conveyor belt” typically occurs between 850
mb
(at the entrance region of the gray arrow) and 200
mb
(the exit region of the gray arrow). It is responsible for providing latent energy for the developing ETCSlide10
Extratropical anticyclones
Just like surface extratropical cyclones develop as areas of low pressure to the east of an upper-level trough axis, surface extratropical
anticyclones can develop as areas of high pressure to the east of an upper-level ridge axisSlide11
Relative importance of different processes to ETC cycle
To conclude this lesson, let’s look at the approximate relative importance of each type of process to the ETC life cycle:Upper-level divergence and vorticity advection (blue curve)Latent heat release from water vapor forming liquid and ice particles (brown curve)
Friction (green curve)
Net effect of all: dashed purple curveSlide12
Where are the ETCs in this analysis of the Pacific Ocean, provided by NOAA Ocean Prediction Center?
What stages are they in? Finally, how do we read/interpret the surface station model?