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METR 2413 31 March 2004

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METR 2413 31 March 2004. Dynamics II: Thermal wind and thermal advection. Review. Hydrostatic balance Ideal gas law p = ρ R d T v , ρ = p / R d T v Take layer average virtual temperature , R and g as constants and integrate LHS. Thickness.

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slide1

METR 2413

31 March 2004

Dynamics II:

Thermal wind and thermal advection

slide2

Review

Hydrostatic balance

Ideal gas law p = ρ RdTv, ρ = p / RdTv

Take layer average virtual temperature , R and g as constants and integrate LHS

slide3

Thickness

So the height difference, z2-z1, between two pressure levels is

where is the average virtual temperature over this layer.

This is called the hypsometric equation for the thickness, z2-z1, between two pressure levels, p1 and p2

Larger thickness means higher mean temperature in the layer.

slide4

Thickness

Example: Thickness of the 1000 hPa to 900 hPa layer

slide5

Thickness

Most common thickness values are:

1000 – 500 hPa, 1000 – 850 hPa, 1000 – 700 hPa

1000 – 500 hPa thickness used to define “bulk” airmass average temperature

1000 – 850 hPa thickness used primarily for snow probability and maximum daytime temperature forecasting

For 1000-500 mb thickness, the 540 dam line (5400 m) is often used as the separator between rain and snow for low terrain

- When there is precip in a region of thickness < 540 dam, it is generally snow

- If thickness > 540 dam, it is usually rain

- Contour intervals are typically 60 m (6 dam)

slide6

Review

Geostrophic wind, pressure gradient force balanced by Coriolis force:

slide7

Thermal wind

In the presence of a horizontal temperature gradient, the tilt of pressure surfaces increases with height.

p=p2

ug

Δz

p=p1

North

cold

warm

slide8

Thermal wind

  • Horizontal temperature gradient
  • Increasing tilt of pressure surfaces with height
  • Increasing pressure gradient force on constant height surfaces with altitude
  • Increasing geostrophic wind with height
  • Vector difference between geostrophic wind at two levels is called thethermal wind.
slide9

Thermal wind

Thermal wind relationship:

The vertical gradient of the geostrophic wind is proportional to the horizontal temperature gradient

slide10

Thermal advection

  • “Advection” – generic term for horizontal transport of some atmospheric property;
  • - typically used in terms of heat transport, but also for moisture
  • To have thermal advection:
  • must have horizontal motion (stronger winds increase thermal advection; little advection under calm conditions)
  • must have horizontal temperature gradient over a large region
  • winds must blow across the zone of strongest horizontal temperature gradient (no advection if wind blows parallel to temperature contours)
slide11

Thermal advection

Warm air advection is occurring in Indiana, cold air advection is occurring over South Dakota and Nebraska

slide12

Thermal advection

  • Warm air advection (WAA) – movement of warmer air toward a fixed point on a horizontal plane; warm air replaces cold air;
  • Low level WAA is common behind warm fronts and ahead of cold fronts
  • Low level WAA can contribute to rising air
  • Cold air advection (CAA) – movement of colder air toward a fixed point on a horizontal plane; cold air replaces warm air
  • Low level CAA is common behind cold fronts
  • Contributes to sinking air
  • Caution: other lifting and sinking mechanisms can complicate rising or sinking due to advection
slide13

Thermal advection

  • Thickness charts often used to infer advection
  • thickness used as proxy for temperature
  • geostrophic wind used as proxy for average air motion
slide14

Thermal advection

  • Thermal wind and thermal advection:
  • Thermal wind – the vector difference between geostrophic flow at 2 different heights (not a real wind!)
  • Thermal wind can be inferred from the thickness field:
  • thermal wind “blows” parallel to the thickness contours, with cold thickness to the left in the Northern Hemisphere
  • Thermal wind rule (in the Northern Hemisphere):
  • if the geostrophic wind backs (turns counterclockwise with height), cold advection is indicated
  • if the geostrophic wind veers (turns clockwise with height), warm advection is indicated
slide16

Thermal advection

  • Can use temperatures at 700 mb as an alternative to thickness:
  • temperature at 700 mb close to 1000 – 500 mb thickness
  • 700 mb wind approximates the movement of the 1000 – 500 mb thickness
  • We can use the geostrophic wind and isotherms at 700 mb to estimate mean lower tropospheric thermal advection:
  • 700 mb thermal advection resembles mean thickness advection below 500 mb
  • spacing of height lines at 700 mb is a measure of wind speed
  • wind direction is parallel to height lines
  • Strength of warm or cold air advection is proportional to the area formed by the intersection of the isotherms and the height contours
slide17

Thermal advection

  • Three factors make thermal advection larger:
  • a strong wind
  • a large temperature gradient
  • a small angle between actual wind direction and temperature gradient (i.e. to maximize heat advection, wind should blow at right angles to isotherms)
  • Very little thermal advection occurs at low latitudes since temperature gradients tend to be very weak.
slide18

Summary

  • Thickness between two pressure levels is proportional to the layer mean temperature
  • Thermal wind – the vector difference between geostrophic wind at 2 different heights, is proportional to the horizontal temperature gradient
  • Thermal advection occurs for horizontal wind blowing across temperature contours
  • If the geostrophic wind backs (veers) with height, cold (warm) advection is indicated
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