SO441 Synoptic Meteorology
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Transcript of SO441 Synoptic Meteorology
SO441 Synoptic Meteorology
Extratropical cyclones
Visible satellite image 26 Oct 2010. Low pressure 955.2 mb. Image courtesy NASA
Cloud pattern typically associated with an extratropical cyclone (Image courtesy NASA)
Extratropical cyclones• What is an extratropical cyclone?– Surface low pressure center associated with upper-level
trough– Most commonly found between 15°-65° latitude
• Where are the extratropical cyclones here?
Where do extratropical cyclones exist?
Cyclone days per winter. Figure from Ulbrich et al. (2009)
Note: the extratropical cyclone track paths tend to follow the areas of greatest surface temperature gradients (land/sea contrasts). This is not by accident.
Process of extratropical cyclone development
• Upper-level trough moves over a front (a surface temperature gradient)– Surface vorticity (spin) usually present along the front– Surface convergence and rising motion yield stretching, which leads to rapid surface vorticity increase
• Air circulation in the lower troposphere around the low pressure, as a result of the increase in surface vorticity, leads to areas of warm-air advection (WAA; ahead of the low) and cold-air advection (CAA; behind the low)– Temperature gradients in the lower troposphere tighten– WAA ahead of the trough axis and CAA behind the trough axis cause the wavelength of the upper-level
trough to shorten (i.e., the trough deepens)• A shorter wavelength trough means greater vorticity advection occurs ahead of the trough axis
– More rising motion, stretching, and enhanced surface convergence ahead of the trough axis• Also latent heat release associated with greater rising motion further deepens the surface low pressure, which feeds
back to even greater WAA and CAA patterns
• However, eventually the upper-level trough “outruns” the surface temperature gradient, and the processes reverse– The surface low pressure fills
• Finally, surface friction is always acting to reverse the process– Acting to reduce surface vorticity
Increase of vorticity of an extratropical cyclone along a front
• From the vorticity equation:
– A. Change in the absolute vorticity at a point on the Earth’s surface– B. Horiztonal advection of absolute vorticity– C. Vertical advection of absolute vorticity – D. Tilting of absolute vorticity – E. Stretching of absolute vorticity – F. Frictional dissipation of absolute vorticity
• Along a front: – Neglect the tilting and friction terms (D and F) (when we say “neglect” in meteorology, we really mean “realize that the
term is usually small compared to the other terms”)
– Re-write the equation in a Lagrangian framework (combine A, B, and C):
• Final result: the change in vorticity following an air parcel is the result of the stretching of vorticity
ya a xa a
BA C ED F
F Fv uVt p x p y p p x y
aa
ddt p
a a aa
d Vdt t p
a aa aV
t p p
Eqn. 1, without D & F
(1)
You learned this in SO335 (Methods) as the “material derivative”, ! aD
Dt
Increase of vorticity of an extratropical cyclone along a front
• From the vorticity equation:
– A. Change in the absolute vorticity at a point on the Earth’s surface– B. Horiztonal advection of absolute vorticity– C. Vertical advection of absolute vorticity – D. Tilting of absolute vorticity – E. Stretching of absolute vorticity – F. Frictional dissipation of absolute vorticity
• Along a front: – Neglect the tilting and friction terms (D and F) (when we say “neglect” in meteorology, we really mean “realize that the
term is usually small compared to the other terms”)
– Re-write the equation in a Lagrangian framework (combine A, B, and C):
• Final result: the change in vorticity following an air parcel is the result of the stretching of vorticity
ya a xa a
BA C ED F
F Fv uVt p x p y p p x y
aa
ddt p
a a aa
d Vdt t p
a aa aV
t p p
Eqn. 1, without D & F
(1)
You learned this in SO335 (Methods) as the “material derivative”, ! aD
Dt
Increase of vorticity of an extratropical cyclone along a front
• Still along a frontal boundary:– Separate variables and integrate the vorticity
equation,
– to get: • This says: the surface absolute vorticity at time t is
equal to the absolute vorticity at the initial time multiplied by an exponential of convergence • When surface air converges, surface vorticity increases
exponentially with time
aa
ddt p
0 expa at t V
Derive this equation for extra credit!
Vp
Hint:
Role of temperature advection in the life cycleof an extratropical cyclone
• Initial trough/ridge pattern moves over a front
• Temperature advection causes the trough to “dig” (slow down), effectively shortening the wavelength and increasing the gradient of vorticity
Ahead of the ridge: cold-air advection
Ahead of the trough: warm advection
Now, in the same space, there are 2 troughs and ridges (wavelength is now ½ of what it was originally)
Role of temperature advection in the life cycle of an extratropical cyclone
• Result of upper-level vorticity gradient is more rising motion– More rising motion at the low center leads to more
convergence• More convergence/rising motion increases surface vorticity (via
stretching)– Increased surface vorticity causes even more temperature advection
» Temperature advection feeds back to even larger upper level vorticity gradient
Example from 16-17 Feb 2003
0000Z 16 Feb 2003
Example from 16-17 Feb 2003
0000Z 16 Feb 2003
• Weak frontal boundaries over Southeast U.S.
• Upper-level trough moves overhead
Example from 16-17 Feb 2003
L
H
Example from 16-17 Feb 2003
L
H
Warm-air advection
Cold-air advection
• Lowest height: 5570 m
Example from 16-17 Feb 2003
1200Z 16 Feb 2003
Example from 16-17 Feb 2003
1200Z 16 Feb 2003
• Surface low has translated northeast & deepened 1-2 mb
• Greater temperature advection causes upper-level trough to dig
Example from 16-17 Feb 2003
0000Z 17 Feb 2003
Example from 16-17 Feb 2003
0000Z 17 Feb 2003
• Original low is now filling in over TN/AL
• Very large temperature gradient off U.S. East Coast promoting new low development there
Example from 16-17 Feb 2003
L
H
LWarm-air advectionCold-air
advection
• Upper-level trough is now more intense (lowest height: 5550 m)
Example from 16-17 Feb 2003
1200Z 17 Feb 2003
• New surface low has now deepened along the very large temperature gradient off U.S. East Coast
Example from 16-17 Feb 2003
L
H
L
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Warm-air advectionCold-air
advection
• Upper-level trough is deeper (lowest height 5510 m)
Example from February 2003: heaviest snow ever in Baltimore
Image of Downtown Annapolis (Main St.) from http://www.weatherbook.com/snow2003.html
Idealized example of this feedback process
• At (a)– Upper-level vorticity maximum, and associated rising motion / stretching / and warm-air advection ahead
of the trough axis (cold-air advection behind it), move over a surface front along the East Coast• At (b), 12 hours later
– The very strong temperature gradient along the coastal front rapidly accelerates temperature advection (warm-air advection ahead of the trough axis, cold-air advection behind it), which increases the height gradient and wind speeds behind the trough axis, which together cause the upper-level trough to “dig”
– The stronger upper-level trough now has even more upper-level vorticity advection associated with it, which causes even more rising motion ahead of the trough axis, which accelerates surface convergence and the increase of surface vorticity, which increases temperature advection, and the process continues…
Summary: extratropical cyclone growth
• In this chapter, we have seen several key themes:– Strong feedbacks between upper-levels and surface
• Surface vorticity growth: surface convergence and column stretching• Lower-level temperature advection shortens wavelength of the trough, increasing
the vorticity gradient– Upper-level vorticity gradient
• Larger the gradient, more intense the rising motion (and thus more surface convergence and column stretching)
– In the real atmosphere, all of these processes occur simultaneously in a “messy” environment• Some contribute to the growth of the cyclone (positive feedbacks)
– Surface convergence, low-level temperature advection, latent heat release, and gradient of upper-level vorticity
• Others contribute to the decay of the cyclone (negative feedbacks)– Surface friction, topography, and phase speed of upper-level trough (the trough will “outrun”
the surface low, eventually placing the surface low beneath a ridge)