1. Chapter 5 – Atmospheric Moisture

2. Atmospheric Moisture Recall: The Hydrologic Cycle

3. Water Vapor Saturation – air that contains as much water vapor as possible (at a given temperature) such that additional water vapor would result in condensation

4. Water Vapor Saturation – air that contains as much water vapor as possible (at a given temperature) such that additional water vapor would result in condensation Unsaturated – air that contains less water vapor (at a given temperature) than possible

5. Water Vapor Saturation – air that contains as much water vapor as possible (at a given temperature) such that additional water vapor would result in condensation Unsaturated – air that contains less water vapor (at a given temperature) than possible Supersaturation – air that contains more water vapor than possible (at a given temperature)

6. Water Vapor Vapor Pressure – The portion of total pressure exerted by water vapor

7. Water Vapor vs. Ice/Water Evaporation – The transition of liquid molecules into the gaseous phase (water in a bowl disappears)

8. Water Vapor vs. Ice/Water Evaporation – The transition of liquid molecules into the gaseous phase (water in a bowl disappears) Condensation – The transition of gaseous molecules into the liquid phase (beads of water on a cold pipe)

9. Water Vapor vs. Ice/Water Evaporation – The transition of liquid molecules into the gaseous phase (water in a bowl disappears) Condensation – The transition of gaseous molecules into the liquid phase (beads of water on a cold pipe) Sublimation – The transition of solid molecules into the gaseous phase (an ice museum vanishes)

10. Water Vapor vs. Ice/Water Evaporation – The transition of liquid molecules into the gaseous phase (water in a bowl disappears) Condensation – The transition of gaseous molecules into the liquid phase (beads of water on a cold pipe) Sublimation – The transition of solid molecules into the gaseous phase (an ice museum vanishes) Deposition – The transition of gaseous molecules into the solid phase (frost on a cold morning)

11. Evaporation and Condensation 2 independent, competing effects 1) Rate of evaporation depends on temperature only

12. Evaporation and Condensation 2 independent, competing effects 2)Rate of condensation depends on vapor pressure only

13. Evaporation and Condensation 2 independent, competing effects - Eventually rate of evaporation = rate of condensation Saturation (and saturation vapor pressure)

14. Vapor Pressure Key ideas: 1) Vapor pressure indicates how much water vapor is in the air

15. Vapor Pressure Key ideas: 1) Vapor pressure indicates how much water vapor is in the air 2) Saturation vapor pressure indicates how much water vapor could be in the air (depends on temperature)

16. Saturation Vapor Pressure

17. Seeing your breath is explained by this curve (as is teakettle steam and steam fog)

18. Useful Indices of Atmospheric Water Vapor Content Vapor pressure – the portion of total pressure exerted by water vapor (mb) Saturation vapor pressure – the vapor pressure at saturation (mb)

19. Useful Indices of Atmospheric Water Vapor Content Vapor pressure – the portion of total pressure exerted by water vapor (mb) Saturation vapor pressure – the vapor pressure at saturation (mb) Specific humidity – the mass of water vapor in a given mass of air (g/kg) = = m q mvmv m v + m d mvmv

20. Useful Indices of Atmospheric Water Vapor Content Vapor pressure – the portion of total pressure exerted by water vapor (mb) Saturation vapor pressure – the vapor pressure at saturation (mb) Specific humidity – the mass of water vapor in a given mass of air (g/kg) = = Saturation specific humidity – the specific humidity at saturation (g/kg) m q mvmv m v + m d mvmv

21. Useful Indices of Atmospheric Water Vapor Content Mixing ratio – the mass of water vapor per mass of dry air (g/kg) = r m d mvmv

22. Useful Indices of Atmospheric Water Vapor Content Mixing ratio – the mass of water vapor per mass of dry air (g/kg) = Saturation mixing ratio - the mixing ratio at saturation (g/kg) r m d mvmv

23. Useful Indices of Atmospheric Water Vapor Content Relative humidity – the amount of water vapor in the air relative to the maximum possible amount of water vapor in the air (%) = RH q s q X 100 q = specific humidity q s = saturation specific humidity

24. Relative Humidity

25. Interesting tidbits RH doesn’t tell you the amount of water vapor in the air

26. Relative Humidity Interesting tidbits RH doesn’t tell you the amount of water vapor in the air RH does tell you the “evaporative” power of the air

27. Relative Humidity Interesting tidbits RH doesn’t tell you the amount of water vapor in the air RH does tell you the “evaporative” power of the air Explains why people need humidifiers indoors in cold climates

28. Relative Humidity

30. Useful Indices of Atmospheric Water Vapor Content Dew Point – the temperature to which air must be cooled to reach saturation

31. Useful Indices of Atmospheric Water Vapor Content Dew Point – the temperature to which air must be cooled to reach saturation The dew point tells you how much water is in the air

32. Useful Indices of Atmospheric Water Vapor Content Dew Point – the temperature to which air must be cooled to reach saturation The dew point tells you how much water is in the air The dew point reveals the “evaporative” power of the air through the dew point depression

33. Dew Point T = Td Saturation T > Td Not saturated

34. Dew Point – Exposing a Myth Have you ever heard somebody say, “It’s 90 degrees with 100% humidity”? They’re lying!!! Here’s Why 1)Dew points are equal to or less than the temperature of their water source 2)The highest dew points occasionally hit the low 80s

35. Dew Point – Exposing a Myth A hot, muggy day Air temperature = 90 o F Dew point = 82 o F

36. Dew Point – Exposing a Myth A hot, muggy day Air temperature = 90 o F Dew point = 82 o F Saturation specific humidity at 90 o F air temperature = 30 g/kg Specific humidity at 82 o F dew point = 24 g/kg

37. Dew Point – Exposing a Myth A hot, muggy day Air temperature = 90 o F Dew point = 82 o F Saturation specific humidity at 90 o F air temperature = 30 g/kg Specific humidity at 82 o F dew point = 24 g/kg RH = 24/30 x 100 = 80%

38. Dew Point – Exposing a Myth A hot, muggy day Air temperature = 90 o F Dew point = 82 o F Saturation specific humidity at 90 o F air temperature = 30 g/kg Specific humidity at 82 o F dew point = 24 g/kg RH = 24/30 x 100 = 80% = 67% if T d is 77 o F

39. Dew Point – Exposing a Myth A hot, muggy day Air temperature = 90 o F Dew point = 82 o F Saturation specific humidity at 90 o F air temperature = 30 g/kg Specific humidity at 82 o F dew point = 24 g/kg RH = 24/30 x 100 = 80% = 67% if T d is 77 o F Myth can be true overnight…

40. Atmospheric Moisture – Key Points How much water vapor could exist Temperature controls how much water vapor can possibly exist in air When the maximum amount of water vapor is in the air, saturation occurs

41. Atmospheric Moisture – Key Points How much water vapor does exist At a given temperature, air can contain an amount of water vapor equal to or less than the amount at saturation Dewpoint reveals how much water does exist in air

42. Moisture Variables 1)Vapor pressure 2)Specific humidity, mixing ratio 3)Relative humidity 4)Dew point

43. Moisture Variables So, at T = 70 o F: Unsaturated air Saturated air Vapor pressure = 14mb Saturation Vapor pressure = 21mb Vapor pressure = 21mb Saturation Vapor pressure = 21mb

44. Moisture Variables So, at T = 70 o F: Unsaturated air Saturated air Vapor pressure = 14mb Saturation Vapor pressure = 21mb Vapor pressure = 21mb Saturation Vapor pressure = 21mb Specific humidity = 9 g/kg Saturation specific humidity = 16 g/kg Specific humidity = 16 g/kg Saturation specific humidity = 16 g/kg

45. Moisture Variables So, at T = 70 o F: Unsaturated air Saturated air Vapor pressure = 14mb Saturation Vapor pressure = 21mb Vapor pressure = 21mb Saturation Vapor pressure = 21mb Specific humidity = 9 g/kg Saturation specific humidity = 16 g/kg Specific humidity = 16 g/kg Saturation specific humidity = 16 g/kg Mixing ratio = 9 g/kg Saturation mixing ratio = 16 g/kg Mixing ratio = 16 g/kg Saturation mixing ratio = 16 g/kg

46. Moisture Variables So, at T = 70 o F: Unsaturated air Saturated air Vapor pressure = 14mb Saturation Vapor pressure = 21mb Vapor pressure = 21mb Saturation Vapor pressure = 21mb Specific humidity = 9 g/kg Saturation specific humidity = 16 g/kg Specific humidity = 16 g/kg Saturation specific humidity = 16 g/kg Mixing ratio = 9 g/kg Saturation mixing ratio = 16 g/kg Mixing ratio = 16 g/kg Saturation mixing ratio = 16 g/kg Relative humidity = 56%Relative humidity = 100%

47. Moisture Variables So, at T = 70 o F: Unsaturated air Saturated air Vapor pressure = 14mb Saturation Vapor pressure = 21mb Vapor pressure = 21mb Saturation Vapor pressure = 21mb Specific humidity = 9 g/kg Saturation specific humidity = 16 g/kg Specific humidity = 16 g/kg Saturation specific humidity = 16 g/kg Mixing ratio = 9 g/kg Saturation mixing ratio = 16 g/kg Mixing ratio = 16 g/kg Saturation mixing ratio = 16 g/kg Relative humidity = 56%Relative humidity = 100% Dew point = 52 o FDew point = 70 o F

48. Dew Point – a Forecasting Tool The dew point is frequently used to forecast nighttime low temperatures – Why?

49. Dew Point – a Forecasting Tool The dew point is frequently used to forecast nighttime low temperatures – Why? 1) Latent heat release during condensation

50. Dew Point – a Forecasting Tool The dew point is frequently used to forecast nighttime low temperatures – Why? 1) Latent heat release during condensation 2) Absorption and re-emission of longwave radiation by cloud droplets

51. Distribution of Water Vapor January July Average Dew Point

52. Measuring Humidity Sling psychrometer – a pair of thermometers, one with moist cotton around the bulb, that are “slung” around until the wet bulb temperature is reached

53. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached

54. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T

55. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T T w is always equal to or greater than the dew point

56. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T T w is always equal to or greater than the dew point Wet bulb depression – the difference between the temperature and the wet bulb temperature

57. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T T w is always equal to or greater than the dew point Wet bulb depression – the difference between the temperature and the wet bulb temperature The wet bulb depression is large for dry air

58. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T T w is always equal to or greater than the dew point Wet bulb depression – the difference between the temperature and the wet bulb temperature The wet bulb depression is large for dry air The wet bulb depression is small for moist air

59. Measuring Humidity Wet bulb temperature (T w ) – the temperature air would have if water was evaporated into it until saturation was reached T w is always equal to or less than T T w is always equal to or greater than the dew point Wet bulb depression – the difference between the temperature and the wet bulb temperature The wet bulb depression is large for dry air The wet bulb depression is small for moist air The wet bulb depression is zero for saturated air

60. Wet Bulb Depression and Swamp Coolers Swamp coolers rely on evaporation to produce cooler air Example: Phoenix, AZ T = 100 o F T d = 37 o F (RH = 12%)

61. Measuring Humidity Aspirated psychrometers – like a sling psychrometer, but has a fan instead of having to be “slung”

62. Measuring Humidity Hair hygrometer – measures humidity based on the expansion and contraction of a strand of hair

63. The Heat Index Heat index – the apparent temperature due to the effects of humidity

64. Condensation in the Atmosphere Condensation is how clouds and fog form

65. Condensation in the Atmosphere Condensation is how clouds and fog form Condensation occurs when air cools below its dew point

66. Condensation in the Atmosphere Condensation is how clouds and fog form Condensation occurs when air cools below its dew point Condensation requires the presence of atmospheric aerosols

67. Condensation and Aerosols Nucleation – the formation of an airborne water droplet by condensation

68. Condensation and Aerosols Nucleation – the formation of an airborne water droplet by condensation Homogeneous nucleation – the formation of water droplets by random collisions of water vapor molecules in the absence of aerosols

69. Condensation and Aerosols Nucleation – the formation of an airborne water droplet by condensation Homogeneous nucleation – the formation of water droplets by random collisions of water vapor molecules in the absence of aerosols Surface tension “squeezes” the water droplet, forcing rapid evaporation

70. Condensation and Aerosols Nucleation – the formation of an airborne water droplet by condensation Homogeneous nucleation – the formation of water droplets by random collisions of water vapor molecules in the absence of aerosols Surface tension “squeezes” the water droplet, forcing rapid evaporation ~400% saturation needed for cloud formation!!!

71. Homogeneous Nucleation A microscopic water droplet Surface tension

72. Homogeneous Nucleation A microscopic water droplet Surface tension Evaporation

73. Condensation and Aerosols Heterogeneous nucleation – the formation of water droplets onto aerosols (condensation nuclei)

74. Condensation and Aerosols Heterogeneous nucleation – the formation of water droplets onto aerosols (condensation nuclei) Aerosols dissolve in water

75. Condensation and Aerosols Heterogeneous nucleation – the formation of water droplets onto aerosols (condensation nuclei) Aerosols dissolve in water Occurs near saturation

76. Condensation and Aerosols Heterogeneous nucleation – the formation of water droplets onto aerosols (condensation nuclei) Aerosols dissolve in water Occurs near saturation Can also occur with large, insoluble aerosols (curvature not a strong effect)

77. Heterogeneous Nucleation A microscopic water droplet (with dissolved aerosol) Surface tension Evaporation

78. Cloud in a Jar Pressurize each jar, wait, and remove lid Water Dust

79. Cloud in a Jar Pressurize each jar, wait, and remove lid Water Dust No Cloud!!Cloud!!

80. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation

81. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature

82. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature 0 o C > T > -4 o C no ice nucleation

83. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature 0 o C > T > -4 o C no ice nucleation -4 o C > T > -10 o C little ice nucleation

84. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature 0 o C > T > -4 o C no ice nucleation -4 o C > T > -10 o C little ice nucleation -10 o C > T moderate ice nucleation

85. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature 0 o C > T > -4 o C no ice nucleation -4 o C > T > -10 o C little ice nucleation -10 o C > T moderate ice nucleation The result is that supercooled water exists as fog and clouds at temperatures between 0 o C and -10 o C

86. Ice Nuclei Ice nucleii – ice look-a-like aerosols on which ice forms at saturation Ice nucleation depends on temperature 0 o C > T > -4 o C no ice nucleation -4 o C > T > -10 o C little ice nucleation -10 o C > T moderate ice nucleation The result is that supercooled water exists as fog and clouds at temperatures between 0 o C and -10 o C Below -10 o C there is a mix of supercooled water and ice

87. Condensation in the Atmosphere Cloud- and fog-forming condensation results from cooling in two forms Diabatic cooling – heat is removed from the air by its surroundings (example – nighttime cooling of surface air)

88. Condensation in the Atmosphere Cloud- and fog-forming condensation results from cooling in two forms Diabatic cooling – heat is removed from the air by its surroundings (example – nighttime cooling of surface air) Adiabatic cooling – no heat is exchanged between the air and its surroundings (example – rising air)

89. Adiabatic Cooling 1 st Law of Thermodynamics: Energy is conserved

90. Adiabatic Cooling 1 st Law of Thermodynamics: Energy is conserved Heat added must equal work done plus a change in internal energy (temperature) ΔH = dw + dq

91. Adiabatic Cooling 1 st Law of Thermodynamics: Energy is conserved Heat added must equal work done plus a change in internal energy (temperature) ΔH = dw + dq However, no heat is exchanged between air and its surroundings with adiabatic processes

92. Adiabatic Cooling 1 st Law of Thermodynamics: Energy is conserved Heat added must equal work done plus a change in internal energy (temperature) ΔH = dw + dq However, no heat is exchanged between air and its surroundings with adiabatic processes Work done must equal change in temperature (0 = dw + dq or dw = -dq)

93. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure

94. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure 2)Air expands (which requires work)

95. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure 2)Air expands (which requires work) 3)Air cools due to work done by air

96. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure 2)Air expands (which requires work) 3)Air cools due to work done by air Sinking air 1)Air encounters higher pressure

97. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure 2)Air expands (which requires work) 3)Air cools due to work done by air Sinking air 1)Air encounters higher pressure 2)Air is compressed (work is done on air)

98. Adiabatic Cooling and Warming Rising air 1)Air encounters lower pressure 2)Air expands (which requires work) 3)Air cools due to work done by air Sinking air 1)Air encounters higher pressure 2)Air is compressed (work is done on air) 3)Air warms due to work done on air

99. Adiabatic Cooling and Warming Dry adiabatic lapse rate – the rate at which unsaturated air cools (warms) as it rises (sinks)

100. Adiabatic Cooling and Warming Dry adiabatic lapse rate – the rate at which unsaturated air cools (warms) as it rises (sinks) = 9.8 o C/km (constant)

101. Adiabatic Cooling and Warming Dry adiabatic lapse rate – the rate at which unsaturated air cools (warms) as it rises (sinks) = 9.8 o C/km (constant) Moist adiabatic lapse rate – the rate at which saturated air cools (warms) as it rises (sinks)

102. Adiabatic Cooling and Warming Dry adiabatic lapse rate – the rate at which unsaturated air cools (warms) as it rises (sinks) = 9.8 o C/km (constant) Moist adiabatic lapse rate – the rate at which saturated air cools (warms) as it rises (sinks) ~ 5 o C/km (variable)

103. Adiabatic Cooling and Warming Dry adiabatic lapse rate – the rate at which unsaturated air cools (warms) as it rises (sinks) = 9.8 o C/km (constant) Moist adiabatic lapse rate – the rate at which saturated air cools (warms) as it rises (sinks) ~ 5 o C/km (variable) Less than the dry adiabatic lapse rate???

104. Dry and Moist Adiabatic Lapse Rates 1km 2km 1km Air temp = 0.2 o C Air temp = 0 o C Air temp = 5 o C Air temp = -9.6 o C Unsaturated Air (9.8 o C/km)Saturated Air (5 o C/km)

105. Adiabatic Cooling and Warming Environmental lapse rate – the rate at which still air changes with height 1km 2km

106. Types of Condensation Dew – condensation of water vapor onto the ground or objects on the ground

107. Dew

108. Types of Condensation Dew – condensation of water vapor onto the ground or objects on the ground Frost – deposition of water vapor onto the ground or objects on the ground

109. Frost

110. Types of Condensation Dew – condensation of water vapor onto the ground or objects on the ground Frost – deposition of water vapor onto the ground or objects on the ground Frozen dew – condensation that freezes

111. Types of Condensation Dew – condensation of water vapor onto the ground or objects on the ground Frost – deposition of water vapor onto the ground or objects on the ground Frozen dew – condensation that freezes Fog – condensation of water vapor onto airborne aerosols, forming a cloud in contact with the ground

112. Types of Condensation Dew – condensation of water vapor onto the ground or objects on the ground Frost – deposition of water vapor onto the ground or objects on the ground Frozen dew – condensation that freezes Fog – condensation of water vapor onto airborne aerosols, forming a cloud in contact with the ground Clouds – condensation of water vapor onto airborne aerosols aloft

113. Fog Radiation fog – fog that forms overnight due to the cooling of air in contact with the ground Associated with temperature inversions Advection fog – fog that forms when warm, moist air moves over a cool surface and cools

114. Advection Fog

115. Fog Upslope fog – fog that forms due to the cooling of air as it rises up a gentle slope Steam fog – fog that forms when warm, moist air mixes with cooler air Precipitation fog – fog that forms when rain evaporates and adds water vapor to ambient air, which then condenses

116. Steam Fog

117. Distribution of Fog in the U.S.