Understanding Cloud Development and Atmospheric Stability

1. Chapter 5 Cloud Development and Precipitation

2. Equlibrium

3. Atmospheric Stability • Air is in stable equilibrium when after being lifted or lowered, it tends to return to its original position – resists upward and downward air motions. • Air Parcel- balloon like blob of air • As air rises its pressure decreases and it expands and cools • As air sinks pressure increases and it is compressed and warms

4. Adiabatic Process • If an air parcel expands and cools, or compresses and warms, with no interchange of heat with its outside surroundings the situation is called an adiabatic process. • Dry Adiabatic lapse rate – 10˚C per 1km or 5.5˚F per 1,000 feet. (applies to unsaturated air) • Moist Adiabatic lapse rate - ~6˚C per 1km or 3.3˚F per 1,000 ft (applies to saturated air). Not a constant. Varies greatly. This number is used to keep things simple.

6. Determining Stability • Determine stability by comparing the temperature of a rising parcel to that of its surrounding environment. • If it is colder than its environment it will be more dense (heavier) and tend to sink back to its original level. This is called stable air because the parcel resists moving away from its original position. • If the parcel is warmer (less dense) than its environment, it will continue to rise until it reaches the same temperature of its environment. This is called unstable air because the parcel continues to move away from its original position.

7. Stable Air • Environmental Lapse Rate – rate at which the air temperature of the environment would be changing if we were to climb upward into the atmosphere. • Absolutely stable – the lifted parcel of air is colder and heavier than air surrounding it (its environment). • Stable air strongly resists upward vertical motion, it will, if forced to rise, tend to spread out horizontally. • Atmosphere is stable when the environmental lapse rate is small – when there is relatively small difference in temperature between the surface air and the air aloft. • The atmosphere stabilizes as the air aloft warms or as the air near the surface cools.

8. Stable Air Dry air example

9. Stable Air Saturated air example

10. Cold surface air, on this morning, produces a stable atmosphere that inhibits vertical air motions and allows fog and haze to linger close to the ground.

11. Unstable Air • Atmosphere is unstable when the air temperature decreases rapidly as we move up into the atmosphere. • Absolutely unstable atmosphere – when considering both moist and dry air – the rising air is warmer than the environmental air around them. • Atmosphere becomes unstable when: • Daytime solar heating of the surface • An influx of warm air brought in by the wind near the surface • Air moving over a warm surface

12. Unstable Air - Dry air example

13. Unstable air. The forest fire heats the air, causing instability near the surface. Warm, less-dense air (and smoke) bubbles upward, expanding and cooling as it rises.

14. Conditionally unstable air.The atmosphere is stable if the rising air is unsaturated...

15. Conditionally Unstable Air • Suppose an unsaturated, but humid air parcel is forced to rise from the surface. • As it rises, it expands and cools at the dry adiabatic rate until it cools to its dew point. • The elevation above the surface where the air is saturated and clouds form is called the condensation level. • Above the condensation level rising air cools at the moist adiabatic rate. • Conditionally unstable atmosphere – the condition for stability being where (if anywhere) the rising air becomes saturated. If unsaturated stable air is lifted to a level where it becomes saturated, instability may result. (See text figure 5.7 on page 116)

16. When the environmental lapse rate is greater than the dry adiabatic rate, the atmosphere is absolutely unstable. When the environmental lapse rate is less than the moist adiabatic rate, the atmosphere is absolutely stable. And when the environmental lapse rate lies between the dry adiabatic rate and the moist adiabatic rate (shaded green area), the atmosphere is conditionally unstable

17. Cumulus clouds developing into thunderstorms in a conditionally unstable atmosphere over the Great Plains. (Note the anvil in the distance)

18. Level of free convection • The level of the atmosphere where an air parcel, after being lifted, becomes warmer than the environment surrounding it. This air can then rise on its own and the atmosphere is unstable.

19. Convection and Clouds • Some areas of the earth surface absorb more sunlight than others, and thus heat up more quickly. (Discuss examples) • Thermal – a hot bubble of air that breaks away from the surface and rises, expanding and cooling as it ascends. • As a thermal rises, it mixes with cooler, drier air aloft and gradually looses its identity. But, if it cools to its saturation point, the moisture inside will condense and the thermal becomes a cumulus cloud.

20. Thermals forming cumulus clouds

23. Four primary means of convection(ways to form clouds) • Surface heating (thermals) • Topographic (forced) lifting • Convergence at the surface • Frontal (forced) lifting

28. Topography and Clouds • Orographic lift – forced lifting along a topographic barrier (mountains) • Rain Shadow – the region on the leeward side of a mountain, where precipitation is noticeably low and the air if often drier • Lenticular clouds – (mountain wave clouds) form on the lee side of mountains. Resemble waves that form in a river downstream from a large boulder. • Rotor clouds – Form beneath lenticular clouds. In the large swirling eddy associated with the mountain wave, the rising part may cool and condense enough to form a cloud.

29. Orographic lift, cloud development, and the formation of a rain shadow

30. The air's stability greatly influences the growth of cumulus clouds.

31. The air's stability greatly influences the growth of cumulus clouds.

32. The air's stability greatly influences the growth of cumulus clouds.

33. The formation of lenticular clouds

34. Lenticular clouds (mountain wave clouds) over Mount Shasta in Northern California

35. Collision and Coalescence Process • In clouds with tops warmer than -15oC collisions between droplets can play a significant role in producing precipitation. • Large drops form on large condensation nuclei or through random collisions of droplets. • As the droplets fall (larger drops fall faster than smaller drops) the larger droplets overtake and collide with smaller drops in their path. • The merging of cloud droplets by collision is called coalescence. (Note: collision does not always guarantee coalescence)

36. Relative sizes of raindrops, cloud droplets and condensation nuclei

37. Collision and Coalescence • In a warm cloud composed only of small cloud droplets of uniform size, the droplets are less likely to collide as they all fall very slowly at about the same speed. Those droplets that do collide, frequently do not coalesce because of the strong surface tension that holds together each tiny droplet.

38. Collision and Coalescence • In a cloud composed of different size droplets, larger droplets fall faster than smaller droplets. Although some tiny droplets are swept aside, some collect on the larger droplet's forward edge, while others (captured in the wake of the larger droplet) coalesce on the droplet's backside.

39. Warm Clouds • A cloud droplet rising then falling through a warm cumulus cloud can grow by collision and coalescence, and emerge from the cloud as a large raindrop.

40. Factors in cloud formation and raindrop production • The cloud’s liquid water content • The range of droplets sizes • The cloud thickness (heaviest precipitation occurs in those clouds with most vertical development) • The updrafts of the cloud • The electric charge of the droplets and the electric field in the cloud

41. Ice Crystal (Bergeron) Process • Process of rain formation proposes that both ice crystals and liquid cloud droplets must co-exist in clouds at temperatures below freezing. • This process is extremely important to rain formation in the middle and high latitudes where cloud tops extend above the freezing level (cold clouds)

42. Supercooled water Collison coalescence occurs here The distribution of ice and water in a cumulonimbus cloud.

43. Ice Nuclei • Ice-forming particles that exist in subfreezing air • Small amount of these available in atmosphere • Clay materials, bacteria in decaying plant leaf material and other ice crystals

44. Saturation Vapor PressureIce vs Water • In a saturated environment, the water droplet and the ice crystal are in equilibrium, as the number of molecules leaving the surface of each droplet and ice crystal equals the number returning. The greater number of vapor molecules above the liquid indicates, however, that the saturation vapor pressure over water is greater than it is over ice.

45. Ice Crystal (Bergeron) Process • The ice-crystal process. The greater number of water vapor molecules around the liquid droplets causes water molecules to diffuse from the liquid drops toward the ice crystals. The ice crystals absorb the water vapor and grow larger, while the water droplets grow smaller. • It takes more vapor molecules to saturate the air directly above the water droplet than it does to saturate the air directly above the crystal. • Ice crystals grow at the expense of the surrounding water droplets.

46. Accretion • In some clouds ice crystals might collide with supercooled liquid droplets. Upon contact, the liquid droplets freeze into ice and stick to the ice crystal – accretion or riming. • The icy matter that forms is called graupel or snow pellets.

47. Secondary Ice particles • In colder clouds the ice crystals may collide with other ice crystals and fracture into smaller ice particles or tiny seeds which freeze hundreds of supercooled droplets on contact.

48. Aggregation • As the crystals fall, they may collide and stick to one another forming an aggregate of crystals called a snowflake.

49. Cloud Seeding • To inject (or seed) a cloud with small particles that will act as nuclei, so that the cloud particles will grow large enough to fall to the surface as precipitation. • First experiments in late 1940s using dry ice. • Silver Iodide is also used today because it’s structure is similar to that of ice crystals. • Natural seeding – cirriform clouds lie directly above a lower cloud deck, ice crystals descend into lower clouds.

50. Natural seeding by cirrus clouds may form bands of precipitation downwind of a mountain chain.