The Greenhouse Effect Solar Radiation, Earth's Atmosphere, and the Greenhouse Effect.
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1 The Greenhouse Effect Solar Radiation, Earth's Atmosphere, and the Greenhouse Effect. Nili Harnik DEES, Lamont-Doherty Earth Observatory
2 Temperature All matter is made up of atoms, which are in constant jiggling motion. Temperature is a measure of the energy which is stored in these motions heat energy. The larger the temperature, the larger the motion of atoms and molecules. The temperature scale which defines the amount of this motion is the Kelvin (absolute temperature). Absolute zero is the state with the least possible energy (almost no motion). The Celsius and Fahrenheit temperature scales are defined based on water boiling and freezing points.
3 Temperature Scales Always use K (Kelvins) in Radiation calculations 0 K = C 0 0 C = 273 K 1 K = 1 0 C T( 0 C)=[ T( 0 F)-32]*5/9
4 Three Aspects of Radiation interacting with matter Transparency - the radiation is unchanged when passing through the medium. Reflection the radiation changes direction when it hits the reflecting medium but otherwise remains the same. Absorption some or all the radiation energy is transferred to the medium. This energy may take a variety of forms, but in general the temperature of the absorbing medium will rise. In a state of equilibrium, this energy will be reemitted, but the wavelength of the emitted radiation will be determined by the absorbing/emitting medium.
5 Absorption of radiation by matter may result in: An increase in the vibrational energy of the molecules of the absorbing medium if it is a solid (temperature rises). Increased molecular velocities, if the absorbing medium is a gas. A chemical change, if the radiant energy is of sufficiently high energy (high frequency) to break chemical bonds or change the energy level of electrons.
6 Radiation absorption by a gas Energetic radiation (UV) can break apart the molecules. Infra-red radiation: can excite rotational and vibrational modes, depending on the nature of the molecule. Asymmetric molecules, with an electric dipole (H 2 O), will absorb more efficiently. Each mode of energy absorption occurs at a specific narrow band of the solar spectrum.
7 Composition of the Atmosphere The Earth's atmosphere contains many trace (or minor) components
8 Interaction of solar radiation with the atmosphere: Reflection: about 20% is reflected by clouds and 5% by the surface, and about 5% is scattered (reflected in many directions) by the atmosphere. Absorption: The most energetic radiation is absorbed high up in the atmosphere, by diatomic oxygen (and nitrogen), resulting in chemical changes breakup of diatomic oxygen to form ozone, and breakup of ozone to form diatomic oxygen again. Transmission: most of the solar radiation, which is in the visible range, is transmitted through the atmosphere. This radiation is absorbed by the Earth.
9 Greenhouse Effect: Absorption by trace gases The major atmospheric components, Nitrogen and Oxygen, absorb little or not radiation. Oxygen absorbs only the most energetic solar radiation (UV). Water vapor absorbs effectively in large sections of the IR wavelength range. CO 2 absorbes in the IR. One of the CO 2 absorption bands overlaps a gap in the water vapor band (referred to as window ). By closing the window, CO 2 increases the absorptive power of the atmosphere. Hence its importance in the climate system.
10 Greenhouse Effect: Absorption by trace gases
11 Absorption by trace gases influences the atmosphere s temperature O 2 + ultraviolet light = O + O O + O 2 = O 3 O 3 + UV light = O 2 + O Effective Temperature
12 Greenhouse Effect X X How big is the greenhouse effect on our planet? Lets do a simple calculation. Lets assume the atmosphere is entirely transparent to the incoming solar flux, and completely absorbs the radiation emitted by the planet
13 Absorption of IR radiation in the atmosphere: The IR radiation emitted by the Earth gradually gets absorbed as it propagates upward. The altitude at which all the radiation gets absorbed is referred to as a unit optical depth. The radiation absorbed by the atmosphere is remitted back in all directions. To simplify matters, we approximate the continuous atmosphere by a thin absorbing sheet, which absorbs all the IR it receives from below, and reemits half of it upward and half downward. The reemitted radiation can get reabsorbed again before it leaves the atmosphere (an optical depth of 2). This would correspond to two absorbing sheets stacked one on top of the other, each absorbing all the radiation it recieves and remitting it equally in both directions.
14 Effect of Atmospheric Absorption: 1 sheet w/o absorption w. absorption α στ g α H=σΤ a atmosphere atmosphere IR absorbing layer στ g (1-α) absorption of solar ground emission of IR (1-α) ground H στ S g = (1-α) 0 στ a = (1-α) στ S g = (1-α) 0 + στ a
15 Effect of Atmospheric Absorption: 1 sheet w/o absorption w. absorption στ S g = (1-α) 0 = 239 Wm -2 στ a = (1-α) The Greenhouse Effect στ S g = (1-α) 0 + στ a στ S g = (1-α) 0 2 Τ g = (1-α) σ Τ g = (1-α) 2σ W/O absorption: T g =255 K or -18 C W. absorption T g =303.5 K or C
16 Radiative Transfer in the Atmosphere Reality is much more complex: Some solar energy is absorbed in the atmosphere. IR absorption happens continually through the troposphere but is not perfect. The surface looses heat not only through radiation, but also through convection (the transfer of heat through turbulent fluid motion), which moves warm and moist air masses from the surface up causing surface sensible and latent heat loss (more on that at later lectures). All this yields a surface temperature of T g =(390/σ) 1/ =288 K=15 C greenhouse effect= =155 Wm -2
17 Annual mean latitudinal distribution of incoming shortwave and outgoing longwave radiation Radiation Wm -2 The total longwave and shortwave radiations are equal in the global average. There is an excess of incoming radiation in the tropical and subtropical regions and a deficit thereof in the middle and high latitudes. Atmospheric motions transfer heat from the equator to the poles.
18 Summary The greenhouse effect results from atmospheric absorption of IR (longwave) radiation emitted from the Earth s surface. IR absorption occurs in broad spectral bands related to molecular motion and energy levels. The major constituent of the atmosphere, Nitrogen (78.01% by volume in dry air), is transparent to both short- and longwave radiation. Oxygen (20.95% by volume) absorbs mainly shortwave (UV) radiation. It is the minor atmospheric constituents, mainly water vapor (about 0.33% of total atmospheric mass and 0.8% by volume) and CO 2 (0.035% by volume) that efficiently absorb the longwave radiation from the Earth s surface. Longwave absorption by the atmosphere strongly reduces the efficiency of Earth s cooling to space, forcing its surface to overheat in order to balance the incoming solar radiation. The end result is a higher surface temperature than the emission temperature of 255 K). At present conditions, the earth has to emit 350 Wm -2 to allow 235 Wm -2 to escape to space and balance the 235 Wm -2 received from the sun. This results in an average surface temperature of 288 K or 15 C
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