- 119 Views
- Uploaded on
- Presentation posted in: General

QG Analysis: Additional Processes

Download Policy: Content on the Website is provided to you AS IS for your information and personal use and may not be sold / licensed / shared on other websites without getting consent from its author.While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server.

- - - - - - - - - - - - - - - - - - - - - - - - - - E N D - - - - - - - - - - - - - - - - - - - - - - - - - -

QG Analysis: Additional Processes

M. D. Eastin

QG Analysis

- QG Theory
- Basic Idea
- Approximations and Validity
- QG Equations / Reference

- QG Analysis
- Basic Idea
- Estimating Vertical Motion
- QG Omega Equation: Basic Form
- QG Omega Equation: Relation to Jet Streaks
- QG Omega Equation: Q-vector Form

- Estimating System Evolution
- QG Height Tendency Equation

- Diabatic and Orographic Processes
- Evolution of Low-level Systems
- Evolution of Upper-level Systems

M. D. Eastin

QG Analysis: Vertical Motion

- Review: The BASIC QG Omega Equation
- Term ATerm BTerm C
- Term B:Differential Vorticity Advection
- Therefore, in the absence of geostrophic vorticity advection and diabatic processes:
- An increase in PVA with height will induce rising motion
- An increase in NVA with heightwill induce sinking motion

- Therefore, in the absence of geostrophic vorticity advection and diabatic processes:

Z-top

Hydrostatic

Balance

Thickness

decreases

must occur

with cooling

PVA

Adiabatic

Warming

Adiabatic

Cooling

Rising

Motions

Sinking

Motions

Z-400mb

PVA

ΔZ

ΔZ decreases

Z-700mb

PVA

ΔZ

ΔZ decreases

Z-bottom

M. D. Eastin

QG Analysis: Vertical Motion

- Review: The BASIC QG Omega Equation
- Term ATerm BTerm C
- Term C:Thermal Advection
- WAA(CAA) leads to local temperature / thickness increases (decreases)
- In order to maintain geostrophic flow, ageostrophic flows and mass continuity
- produce a vertical motion through the layer
- Therefore, in the absence of geostrophic vorticity advection and diabatic processes:
- WAA will induce rising motion
- CAAwill induce sinking motion

Z-top

Z-top

Surface

Rose

Z-400mb

Z-400mb

ΔZ increase

WAA

ΔZ

Surface

Fell

Z-700mb

Z-700mb

Z-bottom

Z-bottom

M. D. Eastin

Vertical Motion: Diabatic Heating/Cooling

- What effect does diabatic heating or cooling have?
- Diabatic Heating:Latent heat release due to condensation (Ex: Cumulus convection)
- Strong surfaces fluxes(Ex: CAA over the warm Gulf Stream)
- (Ex: Intense solar heating in the desert)
- Heating always leads to temperature increases → thickness increases
- Consider the three-layer model with a deep cumulus cloud
- Again, the maintenance of geostrophic flow requires rising motion through the layer
- Identical to the physical response induced by WAA
- Therefore:Diabatic heating induces rising motion

Z-top

Surface

Rose

Z-400mb

ΔZ

ΔZ increases

Surface

Fell

Z-700mb

Z-bottom

M. D. Eastin

Vertical Motion: Diabatic Heating/Cooling

- What effect does diabatic heating or cooling have?
- Diabatic Cooling:Evaporation (Ex: Precipitation falling through sub-saturated air)
- Radiation (Ex: Large temperature decreases on clear nights)
- Strong surface fluxes (Ex: WAA over snow/ice)
- Cooling always leads to temperature decreases → thickness decreases
- Consider the three-layer model with evaporational / radiational cooling
- Again, maintenance of geostrophic flow requires sinking motion through the layer
- Identical to the physical response induced by CAA
- Therefore:Diabatic cooling aloft induces sinking motion

Z-top

Surface

Fell

Z-400mb

ΔZ decreases

ΔZ

Z-700mb

Surface

Rose

Z-bottom

M. D. Eastin

Vertical Motion: Topography

- What effect does flow over topography have?
- Downslope Motions: Flow away from the Rockies Mountains
- Flow away from the Appalachian Mountains
- Subsiding air always adiabatically warms
- Subsidence leads to temperature increases → thickness increases
- Consider the three-layer model with downslope motion at mid-levels
- Again, maintenance of geostrophic flow requires rising motion through the layer
- Identical to the physical response induced by WAA and diabatic heating
- Therefore: Downslope flow induces rising motion

Z-top

Surface

Rose

Z-400mb

ΔZ

ΔZ increases

Surface

Fell

Z-700mb

Z-bottom

M. D. Eastin

Vertical Motion: Topography

- What effect does flow over topography have?
- Upslope Motions: Flow toward the Rockies Mountains
- Flow toward the Appalachian Mountains
- Rising air always adiabatically cools
- Ascent leads to temperature decreases → thickness decreases
- Consider the three-layer model with upslope motion at mid-levels
- Again, maintenance of geostrophic flow requires sinking motion through the layer
- Identical to the physical processes induced by CAA and diabatic cooling
- Therefore:Upslope flow induces sinking motion

Z-top

Surface

Fell

Z-400mb

ΔZ decreases

ΔZ

Z-700mb

Surface

Rose

Z-bottom

M. D. Eastin

QG Analysis: Vertical Motion

- Update: The Modified QG Omega Equation
- + Diabatic + Topographic
- ForcingForcing
- Note: The text includes a modified equation
- with only diabatic effects [Section 2.5]
- Application Tips:
- Differential vorticity advection and thermal advection are the dominant terms
- in the majority of situations → weight these terms more
- Diabatic forcing can be important when deep convection or dry/clear air are present
- Topographic forcing is only relevant near large mountain ranges

Vertical

Motion

Differential Vorticity

Advection

Thermal

Advection

M. D. Eastin

QG Analysis: Vertical Motion

- Application Tips:
- Diabatic Forcing
- Use radar → more intense convection → more vertical motion
- Use IR satellite → cold cloud tops → deep convection or high clouds?
- → warm cloud tops → shallow convection or low clouds?
- Use VIS satellite→ clouds or clear air?
- Use WV satellite→ clear air → dry or moist?

- Topographic Forcing
- Topographic maps→ Are the mountains high or low?
- Use surface winds→ Is flow downslope, upslope, or along-slope?

- Diabatic Forcing

M. D. Eastin

QG Analysis: System Evolution

- Review: The BASIC QG Height Tendency Equation
- Term ATerm BTerm C
- Term B:Vorticity Advection
- Positive vorticity advection (PVA)PVA →
- causes local vorticity increases
- From our relationship between ζg and χ, we know that PVA is equivalent to:

- therefore: PVA → or, since: PVA →
- Thus, we know that PVAat a single level leads toheight falls
- Using similar logic, NVA at a single level leads to height rises

M. D. Eastin

QG Analysis: System Evolution

- Review: The BASIC QG Height Tendency Equation
- Term ATerm BTerm C
- Term C:Differential Thermal Advection
- Consider an atmosphere with an arbitrary vertical profile of temperature advection
- Thickness changes throughout the profile will result from the type (WAA/CAA) and
- magnitude of temperature advection though the profile
- Therefore:An increase in WAA advectionwith height leads to height falls
- An increase in CAA advection with height leads to height rises

M. D. Eastin

System Evolution: Diabatic Heating/Cooling

- Recall:
- Local diabatic heating produces the

- same response as local WAA
- Likewise local diabatic cooling is

- equivalent to local CAA
- Evaluation:
- Examine / Estimate the vertical profile
- of diabatic heating / cooling from all
- available radar / satellite data

Clear Regions

Z

Diabatic Coolingmax

located in upper-levels

due to radiational cooling

Diabatic heatingmax

located near surface

due to surface fluxes

Net Result:Increase in cooling with height

Height Rises

Regions of Deep Convection

Regions of Shallow Convection

Z

Z

Diabatic Heating max

located in upper-levels

due to condensation

Diabatic cooling max

located below cloud base

due to evaporation

Diabatic Coolingmax

located in upper-levels

due to radiational cooling

Diabatic heatingmax

located in lower-levels

due to condensation

Net Result: Increase in heating with height

Height Falls

Net Result: Increase in cooling with height

Height Rises

M. D. Eastin

System Evolution: Topography

- Recall:
- Local downslop flow produces the

- same response as local WAA
- Likewise local upslope flow is

- equivalent to local CAA
- Evaluation:
- Examine / Estimate the vertical profile
- of heating due to topographic effects

Downslope Flow

Upslope Flow

Z

Z

No adiabatic heating

No topographic effects

above the mountains

Adiabatic Heating

due to downslope flow

No adiabatic heating

No topographic effects

above the mountains

Adiabatic Cooling

due to upslope flow

Net Result: Decrease in heating with height

above heating max → height rises

Decrease in heating with height

below heating max → height falls

Net Result: Decrease in cooling with height

above cooling max → height falls

Decrease in cooling with height

below cooling max → height rises

M. D. Eastin

QG Analysis: System Evolution

- The Modified QG Height Tendency Equation
- + Diabatic + Topographic
- ForcingForcing
- Application Tips:
- Differential vorticity advection and thermal advection are the dominant terms
- in the majority of situations → weight these terms more
- Diabatic forcing can be important when deep convection or dry/clear air are present
- Topographic forcing is only relevant near large mountain ranges

Height

Tendency

Vorticity

Advection

Differential Thermal

Advection

M. D. Eastin

QG Analysis: System Evolution

- Application Tips:
- Diabatic Forcing
- Use radar → more intense convection → more vertical motion
- Use IR satellite → cold cloud tops → deep convection or high clouds?
- → warm cloud tops → shallow convection or low clouds?
- Use VIS satellite→ clouds or clear air?
- Use WV satellite→ clear air → dry or moist?

- Topographic Forcing
- Topographic maps→ Are the mountains high or low?
- Use surface winds→ Is flow downslope, upslope, or along-slope?

- Diabatic Forcing

M. D. Eastin

References

Bluestein, H. B, 1993: Synoptic-Dynamic Meteorology in Midlatitudes. Volume I: Principles of Kinematics and Dynamics.

Oxford University Press, New York, 431 pp.

Bluestein, H. B, 1993: Synoptic-Dynamic Meteorology in Midlatitudes. Volume II: Observations and Theory of Weather

Systems. Oxford University Press, New York, 594 pp.

Charney, J. G., B. Gilchrist, and F. G. Shuman, 1956: The prediction of general quasi-geostrophic motions. J. Meteor.,

13, 489-499.

Durran, D. R., and L. W. Snellman, 1987: The diagnosis of synoptic-scale vertical motionin an operational environment. Weather and Forecasting, 2, 17-31.

Hoskins, B. J., I. Draghici, and H. C. Davis, 1978: A new look at the ω–equation. Quart. J. Roy. Meteor. Soc., 104, 31-38.

Hoskins, B. J., and M. A. Pedder, 1980: The diagnosis of middle latitude synoptic development. Quart. J. Roy. Meteor.

Soc., 104, 31-38.

Lackmann, G., 2011: Mid-latitude Synoptic Meteorology – Dynamics, Analysis and Forecasting, AMS, 343 pp.

Trenberth, K. E., 1978: On the interpretation of the diagnostic quasi-geostrophic omega equation. Mon. Wea. Rev., 106,

131-137.

M. D. Eastin