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Dynamic tropopause analysis; What is the dynamic tropopause?. A level (not at a constant height or pressure) at which the gradients of potential vorticity on an isentropic surface are maximized Large local changes in PV are determined by the advective wind
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Dynamic tropopause analysis; What is the dynamic tropopause? • A level (not at a constant height or pressure) at which the gradients of potential vorticity on an isentropic surface are maximized • Large local changes in PV are determined by the advective wind • This level ranges from 1.5 to 3.0 Potential vorticity units (PVUs)
Consider the cross sections that we have been viewing: • Our focus is on the isentropic cross section seen below • the opposing slopes of the PV surfaces and the isentropes result in the gradients of PV being sharper along isentropic surfaces than along isobaric surfaces
Dynamic tropopause pressure: A Relatively high (low pressure) Tropopause in the subtropics, and a Relatively low (high pressure) Tropopause in the polar regions; a Steeply-sloping tropopause in the Middle latitudes
Tropopause potential temperatures (contour interval of 5K from 305 K to 350 K) at 12-h intervals (from Morgan and Nielsen-Gammon 1998) The appearance of the 330 K closed contour in panel c is produced by the large values of equivalent potential temperature ascending in moist convection and ventilated at the tropopause level; as discussed earlier, this is an excellent means of showing the effects of diabatic heating, and verifying models
the sounding shows a tropopause fold extending from 500 to 375 hPa at 1200 UTC, 5 Nov. 1988 for Centerville, AL, with tropospheric air above and extending to 150 hPa. The fold has descended into Charleston, SC by 0000 UTC, 6 November 1988 to the 600-500 hPa layer. The same isentropic levels are associated with each fold
Coupling index: Theta at the tropopause Minus the equivalent Potential temperature at Low levels (a poor man’s lifted index)
December 30-31, 1993 SLP And 925 hPa theta
An example illustrates the detail of the dynamic tropopause (1.5 potential vorticity units) that is lacking in a constant pressure analysis
250 and 500-hPa analyses showing the respective subtropical and polar jets: 250-hPa z and winds 500-hPa z and winds
Dynamic tropopause map shows the properly-sharp troughs and ridges and full amplitudes of both the polar and subtropical jets
The dynamic tropopause animation during the 11 May 1999 hailstorm:
An animation of the dynamic tropopause for the period from December 1, 1998 through February 28, 1999:
The PV Conundrum • IPV (Isentropic Potential Vorticity) maps • Many isentropic surfaces have dynamically significant PV gradients • Hard to know which isentropic surfaces to look at
…identical to the 320 K contour on the 1.5 PVU (tropopause) surface!
Cyclogenesis • Mutual Amplification • Southerlies assoc. w/ upper-level trough intensify surface frontal wave • Northerlies assoc. w/ surface frontal wave intensify upper-level trough • Superposition • Trough and frontal wave approach and occlude
Diabatic Processes • Latent heating max in mid-troposphere • PV increases below LH max • PV decreases above LH max • It’s as if PV is brought from aloft to low levels by latent heating • Strengthens the surface low and the upper-level downstream ridge
Diabatic Processes: Diagnosis • Low-level PV increases • Upper-level PV decreases • Tropopause potential temperature increases
Diabatic Processes: Prediction • Plot low-level equivalent potential temperature instead of potential temperature • Compare theta-e to the potential temperature of the tropopause • If theta-e is higher: • Deep tropospheric instability • Moist convection likely, rapid cyclogenesis