The Earth s Radiation Balance

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2 The Earth s Radiation Balance Incoming Energy = Outgoing Energy (absorbed sunshine)(area) = (thermal loss)(area) S(1-a)pr 2 = s T 4 (4 pr 2 ) Solve for T T = -18 C; (0 F)

3 The radiative equilibrium temperature The equilibrium surface temperature should be -18 C (~0 F). But, the observed surface temperature is +15 C (~60 F). Why? We have an atmosphere

4 Solar Radiation 30% reflected 20% absorbed by the atmosphere ~50% absorbed by the surface

5 Greenhouse Effect Heat radiated by the Earth s surface is absorbed by gases in the atmosphere and reradiated back to the Earth

6 Carbon Dioxide (CO 2 ) Concentrations Combustion of fossil fuels (coal and oil) by humans has increased concentrations of some greenhouse gases

7 Scattering: Why is the sky blue? Sunlight is scattered by air molecules Shorter wavelengths (green, blue, violet) scattered more efficiently Unless we are looking directly at the sun, we are viewing light scattered by the atmosphere Finally, blue dominates over violet because our eyes are more sensitive to blue light

8 The sun appears fairly white when it s high in the sky Near the horizon, sunlight must penetrate more atmosphere and therefore, there is more scattering of blue and other shorter wavelengths The orange sunset occurs because longer wavelengths, such as orange and yellow, make it through If there are a lot of particulates, yellow will be scattered as well Why are Sunsets Red?

9 Weather and Climate What is the difference?

10 Time Scales weather vs climate Weather Hourly The conditions at a specific location at a specific time e.g., this afternoon Diurnal The day-night cycle -24 hours Weekly Standard long range TV weather forecast

11 Climate The average conditions and their variability (includes extremes) Seasonal Annual Decadal Century Geologic Timescales

12 Spatial Terms of Reference Global - The planet as a whole Planetary - as in planetary waves Hemispheric - e.g. northern hemisphere Zonal- implies East-West a latitude band e.g. subtropics o lat Meridional - implies North-South Regional High Plains The Mountains Local Billings

13 Spatial Terms of Reference Synoptic scale 500 to 3000 Kilometers midlatitude cyclones Mesoscale 20 to 200 Kilometers Thunderstorms Microscale centimeters to 1 Kilometer In-Cloud updraft

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15 Seasons & Sun's Distance Figure 3.1 Earth is 5 million kilometers further from the sun in July than in January, indicating that seasonal warmth is controlled by more than solar proximity.

16 Solstice & Equinox At solstice, tilt keeps a polar region with either 24 hours of light or darkness At equinox, tilt provides exactly 12 hours of night and 12 hours of day everywhere Earth's tilt of 23.5 and revolution around the sun creates seasonal solar exposure and heating patterns

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19 Seasons & Solar Intensity Solar intensity, defined as the energy per area, governs Earth's seasonal climate changes A sunlight beam that strikes at an angle is spread across a greater surface area, and is a less intense heat source than a beam impinging directly.

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21 Midnight Sun The region north of the Arctic Circle experiences a period of 24 hour sunlight in summer, where the Earth's surface does not rotate out of solar exposure

22 Take home message Seasons are regulated by the amount of solar energy received at Earth s surface, which depends upon: angle at which sunlight strikes Earth s surface. how many hours the sun shines per day. Seasons are NOT due to the elliptical nature of the earth s orbit, i.e. changes in distance from the Sun.

23 Questions Since the North Pole has 24 hours of sunlight during summer, why isn t it the hottest place on the planet? Why aren t daily temperatures highest on June 15, summer solstice, when the Sun is at its highest and the days are longest?

24 Temperature Lags Earth's surface temperature is a balance between incoming solar radiation and outgoing terrestrial radiation. Peak temperature lags after peak insolation because surface continues to warm until infrared radiation exceeds insolation.

25 Radiation Budget at the top of the Earth s Atmosphere Red Line is incoming radiation from the sun Blue Line is outgoing radiation emitted by the earth

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27 The Job of the Atmosphere is to let the energy out! Piles up in tropics Escapes near poles and aloft The movement of the air (and oceans) allows energy to be transported to its escape zones!

28 What a single cell convection model would look like for a nonrotating earth Thermal convection leads to formation of convection cell in each hemisphere Energy transported from equator toward poles What would prevailing wind direction be over N. America with this flow pattern on a rotating earth?

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30 What s wrong with the 1-cell model? Answer: The Earth Spins and ultimately it is not stable. What is stable?

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34 Climate Zones Circulation features are tied to regional climate Rising air associated with lots of precipitation

35 Climates of the World Deep Tropics: hot and wet, with little seasonal variation Seasonal tropics: hot, with summer rain and winter dry (monsoon) Subtropics: dry and sunny, deserts and savannas, often with a well-defined rainy season (summer or winter) Midlatitude temperate zone: warm summers, cold winters, moisture varies by location but often comes in episodes throughout the year Polar regions: very cold, generally very dry, dark in the winter Other Influences: Ocean currents, continentality, vegetation, mountain ranges (altitude and orographic precipitation) Orographic = lift due to the presence of mountains

36 Coriolis Force acts to the right in the Northern Hemisphere hysics

37 Coriolis Effect The Coriolis Effect deflects moving objects to the right in the northern hemisphere and to the left in the southern.

38 The atmosphere s water

39 The Earth s Hydrologic Cycle

40 Properties of Water Physical States only natural substance that occurs naturally in three states on the earth s surface Heat Capacity Highest of all common solids and liquids Surface Tension Highest of all common liquids Latent Heat of Fusion Highest of all common substances Compressibility Virtually incompressible as a liquid Density Density of seawater is controlled by temperature, salinity and pressure Liquid has maximum density at +4 o C; solid phase has lower density!

41 Molecular Structure of Water water molecule ice Water's unique molecular structure and hydrogen bonds enable all 3 phases to exist in earth's atmosphere.

42 Molecular Structure of Water + + ice - - Water's unique molecular structure and hydrogen bonds enable all 3 phases to exist in earth's atmosphere.

43 Energy associated with phase change 80 calories 100 calories 540 calories!

44 Water vapor pressure Molecules in an air parcel (e.g., N 2, O 2, H 2 O) all contribute to pressure The VAPOR PRESSURE, e, is the pressure exerted by water vapor molecules in the air

45 Water vapor saturation Water molecules move between liquid and gas phases When the rate of water molecules entering the liquid equals the rate leaving the liquid, we have equilibrium The air is said to be saturated with water vapor at this point Equilibrium does not mean no exchange occurs

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50 Expressing the water vapor pressure e = vapor pressure; e s = saturation vapor pressure Relative Humidity (RH) is ratio of actual vapor pressure to saturation vapor pressure 100 * e/e S (e = vapor pressure, e s = saturation vapor pressure) Range: 0-100% (+) Air with RH > 100% is supersaturated RH can be changed by Changes in water vapor content, e Changes in temperature, which alter e S

51 Warm air can hold more water vapor

52 Dewpoint Temperatures Dew point temperature the temperature at which dew forms, i.e. condensation Dewpoint temperature is a measure of the water vapor content of the air It is not a measure of temperature!

53 Condensation Condensation is the phase transformation of water vapor to liquid water Water does not easily condense without a surface present Vegetation, soil, buildings provide surface for dew and frost formation Particles act as sites for cloud and fog drop formation

54 Where do Cloud Condensation Nuclei (CCN) come from? Good CCN are hygroscopic ( like water,) Salt and acid particles in the atmosphere Natural CCN Sea salt (Na +, Cl -, SO 4=, K +, Mg 2+ ) biogenic sulfur emissions vegetation burning CCN from human activity Pollutants from fossil fuel combustion (CO 2, SO 2 )

55 Smog over China

56 Fogs are clouds in contact with the ground Several types of fogs commonly form Radiation fog Advection fog Upslope fog Evaporation (mixing) fog Fogs

57 Clouds Clouds result when air becomes saturated away from the ground They can be thick or thin, large or small contain water drops and/or ice crystals form high or low Clouds impact the environment in many ways Temperature, precipitation (snow/rain), pollutant processing, climate change, kill?, etc.

58 Cloud Classification Clouds are categorized by their height, appearance and vertical development High Clouds - generally above 16,000 ft at middle latitudes Main types - Cirrus, Cirrostratus, Cirrocumulus (wispy; high altitude ice) Middle Clouds 7,000-23,000 feet Main types Altostratus, Altocumulus Low Clouds - below 7,000 ft Main types Stratus, stratocumulus, nimbostratus (layered; stable) Vertically developed clouds (via convection) Main types Cumulus, Cumulonimbus (cottony; beautiful day, but it might rain)

59 Cloud type summary

60 Cirrus

61 Cirrus Cirrus Display at Dawn

62 Stratus from below

63 Stratus from above

64 Stratus over the ocean

65 Puffy cumulus

66 Vertically developed clouds Cumulus Puffy cotton Flat base, rounded top More space between cloud elements than stratocumulus Cumulonimbus Thunderstorm cloud Very tall, often reaching tropopause Individual or grouped Large energy release from water vapor condensation

67 Cumulonimbus

68 Cumulonimbus with Pileaus caps

69 Cumulonimbus Clouds Spawn Tornadoes

70 Cirrocumulus Cirrocumulus at Sunset

71 Altostratus Alto Stratus Castellanus

72 Lenticular clouds downwind of mountains

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75 Stability and Cloud Development

76 Why is stability important? Vertical motions in the atmosphere are largely controlled by vertical stability There are two types of vertical motion: forced motion such as forcing air up over a hill, over colder air, or from horizontal convergence buoyant motion in which the air rises because it is less dense than its surroundings - stability is especially important here

77 Stability & Instability A rock, like a parcel of air, that is in stable equilibrium will return to its original position when pushed. If the rock instead accelerates in the direction of the push, it was in unstable equilibrium.

78 Stability in the atmosphere An Initial Perturbation Stable Unstable Neutral If an air parcel is displaced from its original height it can: Return to its original height - Stable Accelerate upward because it is buoyant - Unstable Stay at the place to which it was displaced - Neutral

79 Lapse rate The lapse rate is the change of temperature with height in the atmosphere There are two kinds of lapse rates: Environmental Lapse Rate (~ 4 /1000 m) What you would measure with a weather balloon Parcel Lapse Rate The change of temperature that an air parcel would experience when it is displaced vertically This is assumed to be an adiabatic process (i.e., no heat exchange occurs across parcel boundary)

80 Stability and the dry adiabatic lapse rate Atmospheric stability depends on the environmental lapse rate A rising unsaturated air parcel cools according to the dry adiabatic lapse rate If this air parcel is warmer than surrounding air it is less dense and buoyancy accelerates the parcel upward colder than surrounding air it is more dense and buoyancy forces oppose the rising motion

81 A saturated rising air parcel cools less than an unsaturated parcel If a rising air parcel becomes saturated condensation occurs Condensation warms the air parcel due to the release of latent heat So, a rising parcel cools less if it is saturated Define a moist adiabatic lapse rate ~ 6 C/1000 m Not constant (varies from ~ 3-9 C) depends on T and P

82 Atmospheric stability depends on the environmental lapse rate A rising saturated air parcel cools according to the moist adiabatic lapse rate When the environmental lapse rate is smaller than the moist adiabatic lapse rate, the atmosphere is termed absolutely stable Recall that the dry adiabatic lapse rate is larger than the moist What types of clouds do you expect to form if saturated air is forced to rise in an absolutely stable atmosphere? Stability and the moist adiabatic lapse rate dry

83 Absolute instability The atmosphere is absolutely unstable if the environmental lapse rate exceeds the moist and dry adiabatic lapse rates This situation is not long-lived Usually results from surface heating and is confined to a shallow layer near the surface Vertical mixing can eliminate it Mixing results in a dry adiabatic lapse rate in the mixed layer, unless condensation (cloud formation) occurs (in which case it is moist adiabatic)

84 Absolute instability (examples)

85 What if the environmental lapse rate falls between the moist and dry adiabatic lapse rates? The atmosphere is unstable for saturated air parcels but stable for unsaturated air parcels This situation is termed conditionally unstable This is the typical situation in the atmosphere Conditionally unstable air