Richard B. Rood (Room 2525, SRB) AOSS 401 Geophysical Fluid Dynamics: Atmospheric Dynamics Prepared: 20131010 Equations of Motion in Pressure Coordinates / Thermal Wind Richard B. Rood (Room 2525, SRB) rbrood@umich.edu 734-647-3530 Cell: 301-526-8572

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Outline Equations of Motion in Pressure Coordinates Thermal wind Revisit the Tour of the Earth Vertical structure

Return to Pressure Coordinates In the coming weeks, we will work mostly with the equations of motion in pressure coordinates We have already derived and used extensively the horizontal momentum equations in p-coordinates Remaining equations: Thermodynamic equation Continuity equation Vertical momentum equation (hydrostatic balance) Plus, what to do with the material derivative?

Our approximated horizontal momentum equations (in p coordinates) No viscosity, no metric terms, no cos-Coriolis terms Subscript h: horizontal Subscript p: constant p surfaces! Sometimes subscript is omitted,  tells you that this is on p surfaces

Geostrophic Wind (in p coordinates) Component form: Vector form: Here we implicitly assume that the partial derivatives in x and y direction are computed on constant p surfaces. Advantage of the p coordinates: Simplicity of the equation! Density no longer appears explicitly.

What do we do with the material derivative? By definition: Example: Total derivative of the temperature on constant z surfaces (subscript omitted)

What do we do with the material derivative when using p in the vertical? By definition: Total derivative DT/Dt on constant pressure surfaces: (subscript omitted)

Think about vertical motion in pressure coordinates For upward motion, what is the sign of ‘w’ (vertical velocity in height coordinates)? What is the sign of ω for upward vertical motion? Remember: And pressure decreases with height… What is the sign of Dp/Dt (change in pressure following the motion) for upward motion? For downward motion?

Think about vertical motion in pressure coordinates Something to keep in the back of your mind… ω is negative for upward motion ω is positive for downward motion

Thermodynamic equation (in p coordinates) From Holton, we can Derive two forms of the thermodynamic equation Expand the material derivative and use

Thermodynamic equation (in p coordinates) Collect terms in ω and divide through by cp Use the equation of state (ideal gas law)

Thermodynamic equation (in p coordinates) Define the static stability parameter Sp What is static stability?

Thermodynamic equation (in p coordinates) If there is no horizontal advection, then the time rate of change of temperature is due to…? Diabatic heating (radiation, condensation) Adiabatic rising/sinking http://www.wunderground.com/modelmaps/maps.asp?model=NAM&domain=US

Continuity equation in z coordinates: in p coordinates: We could try to derive the pressure-coordinate version from the height-coordinate equation (as we did with the pressure gradient force in the horizontal momentum equations), but…

Re-deriving the continuity equation in p coordinates It turns out to be easier to re-derive it from mass conservation x y z Start with an air parcel with volume: V= x y z Apply the hydrostatic equation p= -gz to express the volume element as V= - x y p/(g) The mass of this fluid element is: M = V= -  x y p/(g) = - x y p/g

Re-deriving the continuity equation in p coordinates x y z (M = - x y p/g) Use the product rule Differential calculus Take the limit Continuity equation in p coordinates

Continuity equation(in p coordinates) This form of the continuity equation contains no reference to the density field and does not involve time derivatives. The simplicity of this equation is one of the chief advantages of the isobaric system. Ease of computing vertical motion from convergence/divergence is another…

Hydrostatic equation (in p coordinates) Hydrostatic equation in z-coords Rearrange (and assume g constant) Apply the equation of state Replaces the vertical momentum equation

Approximated equations of motion in pressure coordinates

In the derivation of the equations in pressure coordinates: Have used conservation principles. Have relied heavily on the hydrostatic assumption. Required that conservation principles hold in all coordinate systems. Plus we did some implicit scaling (metric terms, cosine coriolis terms dropped out).

The thermal wind Connecting horizontal temperature structure to vertical wind structure in a balanced atmosphere

Equations of motion in pressure coordinates (plus hydrostatic and equation of state)

Geostrophic wind

Hydrostatic Balance

Schematic of thermal wind. Thickness of layers related to temperature. Causing a tilt of the pressure surfaces. from Brad Muller

What is a tactic for exploring vertical behavior?

Geostrophic wind Take derivative wrt p. Links horizontal temperature gradient with vertical wind gradient.

Thermal wind p is an independent variable, a coordinate. Hence, x and y derivatives are taken with p constant.

A excursion to the atmosphere. Zonal mean temperature - Jan approximate tropopause south (summer) north (winter)

A excursion to the atmosphere. Zonal mean temperature - Jan ∂T/∂y ? south (summer) north (winter)

A excursion to the atmosphere. Zonal mean temperature - Jan ∂T/∂y ? <0 <0 <0 <0 >0 <0 south (summer) north (winter)

A excursion to the atmosphere. Zonal mean temperature - Jan ∂T/∂y ? ∂ug/∂p ? <0 >0 <0 <0 >0 <0 <0 <0 > 0 >0 >0 <0 south (summer) north (winter)

A excursion to the atmosphere. Zonal mean wind - Jan south (summer) north (winter)

Relation between zonal mean temperature and wind is strong This is a good diagnostic – an excellent check of consistency of temperature and winds observations. We see the presence of jet streams in the east-west direction, which are persistent on seasonal time scales. Is this true in the tropics?

Thermal wind

Thermal wind

Thermal wind

Thermal wind ?

From Previous Lecture Thickness Note link of thermodynamic variables, and similarity to scale heights calculated in idealized atmospheres Z2-Z1 = ZT ≡ Thickness - is proportional to temperature is often used in weather forecasting to determine, for instance, the rain-snow transition.

Similarity of the equations There is clearly a relationship between thermal wind and thickness.

Schematic of thermal wind. Thickness of layers related to temperature. Causing a tilt of the pressure surfaces. from Brad Muller

Another excursion into the atmosphere. 850 hPa surface 300 hPa surface from Brad Muller

Another excursion into the atmosphere. 850 hPa surface 300 hPa surface from Brad Muller

Another excursion into the atmosphere. 850 hPa surface 300 hPa surface from Brad Muller

Another excursion into the atmosphere. 850 hPa surface 300 hPa surface from Brad Muller

Summary of Key Points The weather and climate of the Earth are responses to basic attributes (geometry) of energy sources. The patterns of weather and climate that we see are not random or accidental. Basic redistribution of energy Determined by characteristics of Earth – especially relation of Earth to Sun and rotation Determined by geography Determined by surface energy characteristics Dynamics of atmosphere and ocean, though complex, organize the air and water into features that we can characterize quantitatively  and predict There is strong consistency between energy, thermodynamic variables, and motion (momentum)