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Understanding Adiabatic Heating and Cooling Near Topographic Barriers

Adiabatic heating and cooling near topographic barriers can have significant effects on local climate. Downslope flow leads to warming, while upslope flow results in cooling. This phenomenon is observable worldwide and is known as the Chinook Wind in the Rockies and the Foehn Wind in Europe. The adiabatic lapse rate of 9.8°C per km plays a key role in these temperature changes. Learn more about this atmospheric process with examples like Brookings in the Northwest.

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Understanding Adiabatic Heating and Cooling Near Topographic Barriers

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  1. Adiabatic heating/cooling • Can be VERY significant near topographic barriers • Warming with downslope flow • Cooling with upslope flow.

  2. Downslope Warming • Large warming during downslope flow • Often large over Cascade foothills (e.g., Cascades-North Bend), but apparent all over the world, including to the lee (east) of the Rockies--the Chinook Wind. • In Europe called the Foehn Wind. • Usually, air comes from mid-levels where potential temperature is higher than at the surface. A drop in dew point usually accompanies downslope flow.

  3. Brookings: The Classic Northwest Example

  4. Adiabatic cooling • Air escaping from bicycle tire • Exiting an aerosol can • Rising air in the atmosphere

  5. Adiabatic lapse rate • As we will see, with no moist processes, air warms by 9.8 C per km due to adiabatic compression and cools by the same rate. • Called the adiabatic lapse rate.

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