Introduction to Isentropic Coordinates:! a new view of mean meridional & eddy circulations" Cristiana Stan
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1 Introduction to Isentropic Coordinates:! a new view of mean meridional & eddy circulations" Cristiana Stan School and Conference on the General Circulation of the Atmosphere and Oceans: a Modern Perspective! July 11-15, 2011! ICTP-Trieste, 1! Italy!
2 Mean Meridional Circulation Mechanism for the meridional transports of energy and moisture in the atmosphere 2!
3 What mathematical model do we use to represent " these observed features?"! The heating processes at work in the atmosphere are very complicated, and motiondependent. The heating is very closely related to moist processes, including cloud formation and precipitation, radiation, and diffusion.! The response of the atmospheric circulation to the heating is complicated because of the existence of eddies and their interaction with the mean flow. These eddies are neither purely random, nor purely regular. 3!
4 Introduction" The vertical stratification of the atmosphere can be represented using various coordinates such as:!physical height, z -coordinate: height above the Earth's surface!pressure, p -coordinate: atmospheric pressure!sigma, ; where p is the air pressure and ps is the surface-air pressure!potential temperature, ; where T is the air temperature, p0 = 100 kpa, and. 4!
5 Review of Potential Temperature Properties"!!Physical Interpretation is the temperature of a material element would have if it were adiabatically* expanded (for p > p0) or compressed (for p < p0) to the reference pressure p0.!!materially conserved for adiabatic flow Considering air to be an ideal gas, so that obeys the ideal gas law, then the first law of thermodynamics can be written: (2) *without heating 5!
6 (2) using the logarithm s property, (2) can be written as (3) and we can write (3) as (4) Written in terms of potential temperature, (4) becomes When, the flow is termed adiabatic and. Thus the potential temperature is materially conserved* for adiabatic flow. * 6! 6!
7 Transformation of the Quasi-static Primitive Equation " to Isentropic Coordinate " Using the longitude, the latitude, and the physical height z as the independent spatial coordinates, the quasi-static primitive equations for inviscid, adiabatic flow are: (1) (2) (3) (4) 7!
8 (5) (6) with the material derivative: (7) Transformation to coordinates: 8!
9 1.!Material Derivative (7) 9!
10 2.!Continuity Equation (4) To transform we first note that 10!
11 To transform we first note that hydrostatic equation (3) where the pseudo-density, is defined by 11!
12 3.!Pressure Gradient Force using definition of potential temperature we can write using the ideal gas law we can write 12!
13 where is the Montgomery potential. 13!
14 4.!Hydrostatic equation (3) where is the Exner function. 14!
15 The quasi-static primitive equations in isentropic coordinates where is the pseudo-density, the Montgomery potential, the Exner function, and 15!
16 Zonal Mean Departure from the Zonal Mean or eddy component Statistics of interest Eddies alternating trains of low and high pressure systems moving in circular motions in the westerly flow push the warm air from the subtropics poleward and cool air from high latitudes equatorward; the net effect is a reduction of equator-to-pole temperature gradient transport also momentum and the eddy momentum flux influences the zonal mean temperature through the thermal wind balance that dominates the middle latitudes. total flux symmetric circulation flux due to eddies 16!
17 The Zonal Mean Equations in Isentropic Coordinates 17!
18 Transform the quasi-static primitive equations in isentropic coordinates in flux form 18!
19 19!
20 Define a mass-weighted zonal mean 20!
21 where denotes the divergence of the Eliassen-Palm flux,. 21!
22 Mean Meridional Circulation! heating induces a meridional circulation, i.e., implies that.! meridional mass convergence (divergence) requires an increase (decrease) of the upward mass flux with height in regions of cooling. Mass stream function: which satisfies the equations: 22!
23 Mean Meridional Mass Stream Function, Tropospheric Perspective 23!
24 Mean Meridional Mass Stream Function, Stratospheric Perspective 24!
25 25! Diabatic heating
26 barotropic wave baroclinic wave pressure torque exerted by the fluid above an isentrope on that below. 26!
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