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CHAPTER 5 CLOUDS AND STABILITY. Adiabatic processes. Remember that rising air expands and cools, and sinking air compresses and warms When this happens in unsaturated conditions, it is called an adiabatic process – no heat is gained or lost - PowerPoint PPT Presentation
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CHAPTER 5
CLOUDS AND STABILITY
CHAPTER 5
CLOUDS AND STABILITY
Remember that rising air expands and cools, and sinking air compresses and warms
When this happens in unsaturated conditions, it is called an adiabatic process – no heat is gained or lost
This is reversible – the air parcel has the same temperature at the beginning and end
But what happens if at some point along its path the parcel becomes saturated, and a cloud forms? (more on this in a minute…)
Simple definition: the condition is stable if an object, when forced to move, will tend to move back to its original position
If it tends to continue moving away from its original position, it is unstable
In atmospheric science, we often consider the motions of air parcels, which can heat and cool but do not mix in air from the outside
Rising parcels expand and cool, sinking parcels are compressed and warm
At the same height, warm air is less dense than cool air
An unsaturated (dry) parcel will always rise and sink at 9.8°C per km – the dry-adiabatic lapse rate
For the sake of discussion today, we’ll just use the round value of 10 °C per km for the dry-adiabatic lapse rate
Stepped Art
Fig. 5.2, p. 123
Moist parcels• When parcels rise and cool, they will
eventually become saturated• As they continue to rise, the water vapor will
condense into liquid water – a cloud• Remember what happens during
condensation: latent heat is released inside the parcel
• So, instead of cooling at 10°C per km, it cools slower – usually around 6°C per km – this is the moist-adiabatic lapse rate
Table 5.1, p. 123
Parcels (individual bubbles of air) always rise and sink at either the dry or moist adiabatic rate
The environment (the air surrounding the parcel) can have a variety of temperature profiles
This environmental rate is measured with radiosondes (on weather balloons)
Since the adiabatic lapse rates are known, we can compare them to the environmental lapse rate to determine whether the parcel will be stable or unstable◦ If a parcel is forced to rise, and it’s warmer than its
environment, it will continue to rise: unstable◦ If it is forced to rise and is cooler than its
environment, it will sink back down to the original position: stable
When the environmental lapse rate is less than the moist adiabatic rate (6°C/km) ◦ All parcels will be colder than their environment
and sink back to their original position Example: temperature inversion
(temperature increases with height) – acts as a lid
Often occurs at night due to radiational cooling
When environmental lapse rate equals the dry-adiabatic lapse rate
Unsaturated parcels will not tend to rise or sink in this condition – they tend to stay where they are
If environmental lapse rate equals moist-adiabatic lapse rate, then the atmosphere is neutrally stable for saturated parcels
When the environmental lapse rate is greater than the dry-adiabatic lapse rate◦ All parcels will be warmer than their environment
and continue to rise This condition usually only occurs near the
surface, and not for very long – the rising parcels will bring the warm air up and cool air will mix down around them
No need for a helicopter here!But this would also never happen!
When the environmental lapse rate is between the dry and moist adiabatic lapse rates◦ Unsaturated parcels will sink back to their original
position, saturated parcels will continue to rise There is instability, on the condition
that the parcel is saturated On average, the atmosphere is in this state
(average environmental lapse rate = 6.5°C/km)
This helps to explain why cumulus clouds can grow very tall (into cumulonimbus) – only saturated parcels continue to rise
Need the helicopter here But not here
Fig. 5.10, p. 130
Warming at low levels or cooling aloft: increases lapse rate, makes atmosphere less stable◦ “Warm air advection” at low levels will destabilize
the atmosphere Mixing
◦ If absolutely unstable, mixing will make atmosphere more stable
◦ If stable, mixing can make atmosphere unstable Lifting or subsidence in layers
If a whole layer sinks, it compresses in the If a whole layer sinks, it compresses in the denser air near the ground, top warms denser air near the ground, top warms more than bottom, and becomes more more than bottom, and becomes more stablestable
If a whole layer rises, it stretches in the less-If a whole layer rises, it stretches in the less-dense air aloft, and it tends to become more dense air aloft, and it tends to become more unstable, especially when the bottom is unstable, especially when the bottom is saturated and the top is dry – saturated and the top is dry – convective convective instabilityinstability
In real life, we don’t have helicopters pulling parcels of air up and down…so what causes air to rise and sink?
Lifting Condensation Level (LCL) : level at which condensation occurs – this represents the cloud base◦ Force an unsaturated parcel to
rise from the surface◦ Temperature will decrease by 10
°C per km, dew point by 2 °C per km until saturated
◦ At the point where the T and Td are equal, the parcel is saturated, water can condense, and a cloud can form (T and Td will fall at the same rate above this)
◦ Handy formula: LCL = 125 (T-Td), where T and Td are in Celsius, and LCL will be in meters
Stepped Art
Fig. 5.16, p. 134
Level of Free Convection (LFC) : level at which air will continue to rise without forcing◦ Force an unsaturated parcel
to rise from the surface◦ Calculate how the
temperature cools with height (using dry adiabatic rate when unsaturated, moist adiabatic when saturated)
◦ Find the point where the parcel’s temperature becomes warmer than its environment – above this point, it will rise freely
Equilibrium level (EL): level above the LFC at which the air will stop rising◦ Continue the process that you used for the LFC
and find the point at which the parcel’s temperature becomes equal to or cooler than the environmental temperature
If the atmosphere is very unstable, this level can be very high, and this situation is conducive to deep cumulonimbus development
Nashville, TN Nashville, TN North Platte, NENorth Platte, NE
Nashville, TN Nashville, TN North Platte, NENorth Platte, NE
Mountains can provide the lifting required to bring air to its LCL and/or LFC
On the windward side, clouds often form and rain/snow is common
On the leeward side there is sinking motion – a “rain shadow”
If unsaturated, temperature will be the same at start and finish
But if saturation is reached…this is no longer reversible
Heat is released in condensation
In stable conditions above a mountain, waves can set up in the airflow
Clouds can form on the upward parts of the waves, and they appear to be stationary (standing wave clouds)
They sometimes take a “flying saucer” appearance
Lenticular wave clouds
SPECIAL TOPIC
• Subsidence Inversions– Strong subsidence exacerbates air pollution due to the lack of
vertical motion – Pollution is not diluted
FOCUS
• Lake Effect Snow (Great Lakes)– Snowstorms that form on the downwind side of
one of these lakes are known as lake effect snows
– Cold air moves over the lakes when they are relatively warm and not quite frozen
– Water vapor absorbed– Becomes snow on edge of lake
• Rising motion due to heat addition and slowing/terrain
Lake Effect Snow
CLOUD DEVELOPMENT
• Changing cloud forms– Stratus clouds can change to cumulus clouds
if the top of the cloud cools and the bottom of the cloud warms
– Altocumulus castellanus: castle-like towers on altocumulus
– If moist stable air without clouds is mixed or stirred it can form stratocumulus clouds.
Fig. 5.25, p. 140
Fig. 5.26, p. 141