Presentation is loading. Please wait.

Presentation is loading. Please wait.

Lesson 2 AOSC 621. Radiative equilibrium Where S is the solar constant. The earth reflects some of this radiation. Let the albedo be ρ, then the energy.

Similar presentations

Presentation on theme: "Lesson 2 AOSC 621. Radiative equilibrium Where S is the solar constant. The earth reflects some of this radiation. Let the albedo be ρ, then the energy."— Presentation transcript:

1 Lesson 2 AOSC 621

2 Radiative equilibrium Where S is the solar constant. The earth reflects some of this radiation. Let the albedo be ρ, then the energy absorbed by the earth is (1- ρ)F s. The thermal energy emitted by the earth is σ B T e 4 Hence we get

3 Radiative equilibrium The spherical albedo of the earth is about 30%. This gives an effective temperature of 255 K. This is considerably lower than the measured average temperature at the surface T s of about 288 K. The fact that T s >T e is seen in all of the terrestrial planets with substantial atmospheres. It is due to the fact that whereas the planets are relatively transparent in the visible part of the spectrum, they are relatively opaque in the infra-red. A portion of the IR emitted by the surface and atmosphere is absorbed by polyatomic gases and re- emitted in all directions – including back to the earth.

4 Greenhouse effect - one atmospheric layer model  is the fraction of the IR radiation absorbed by the atmosphere

5 Greenhouse effect

6 An examination of the previous equation shows that as e increases the ground temperature increases. This is what is referred to as greenhouse warming. As we shall show later, not all of the additional energy trapped by the additional absorption goes inot heating the surface. Some, for example goes into evaporation of water - which stores energy in the atmosphere as additional latent heat. So one should view the inference of the equation with some caution. This issue will be discussed later when climate feedback is addressed.

7 Radiative equilibrium First Law of Thermodynamics - the time rate of change of the column energy is and Where N is called the radiative forcing Where Teff is the effective transmission of the atmosphere to thermal radiation ( (1-e) in the simple model)

8 Perturbation to the radiative forcing What happens if N(T S ) is changed by Δ N(T S ) Assume that the atmosphere moves to a new equilibrium temperature, then we can write We define the climate sensitivity α as

9 Climate sensitivity

10 CO 2 doubling The calculated radiative forcing from doubling CO 2 is ~4 Wm -2 Assuming that the solar flux is constant we get F TOA = 240 Wm -2 and T s = 288 K, hence α=0.3 Wm -2 K -1 Hence the increase in surface temperature is 1.2 K

11 Change in the solar constant Suppose the solar constant were to decrease by 1% Assume no feedbacks other than the reduced thermal emission. If there is no albedo change due to the decreased solar flux then the second term in the climate sensitivity is zero. Hence we get:

12 Change in the solar constant 2 Substituting for F TOA Change in temperature is -0.72 K

13 General expression for α Consider a parameter Q ( such as albedo) that depends on the surface temperature The direct forcing ΔN is augmented by a term Solving for the climate sensitivity we find

14 General expression for α If we have an arbitrary number of forcings Q then one can derive a general expression for the climate sensitivity It should be noted that the above equation assumes that the individual forcings are independent of one another

15 Radiative forcing of greenhouse gases

16 Radiative forcing

17 Negative feedback

18 Positive feedback

19 Polar ice coverage - positive feedback


21 Fig. 7-27, p. 191 Positions of the jet streams

22 Fig. 8-30, p. 231 Relation between jet stream and high and low pressure systems

23 Using Total Ozone measurements Contributions to the column ozone amount (total ozone) come mainly from the lower stratosphere. In this altitude region ozone has a long chemical lifetime compared to its dynamic lifetime. Hence one can treat Total Ozone acts as a dynamic tracer. The subtropical and polar fronts correspond to a rapid change in the tropopause height, and total ozone shows abrupt changes. Hudson et. al, 2003, 2006 developed a method to determine the position of the fronts (jet streams) from satellite total ozone data.

24 Jet Streams on March 11, 1990 Sub-tropical = Blue, Polar = Red

25 Mean latitude of the Sub-tropical front Shift from 1980 to 2004 is 1.7 degrees

26 Mean Latitude of the Polar Front Shift from 1980 to 2004 is 3.1 degrees

27 Summary of values of the tropical belt expansion Zonal mean stream function study gives values from 2.5 to 3.1 degrees Tropopause analysis gives values of 5-8 degrees OLR study gives values from 2.3 to 4.5 Ozone gives value for the Northern Hemisphere only of 1.7 degrees All over the period 1979 to 2005

28 21 st Century Predicted Widening Ensemble mean ~2 deg. latitude Lu et al. (2007)

29 Observed vs Predicted Widening Observed: ~2-5°latitude 1979-2005 Modeled (A2 scenario): ~2°lat over 21 st century Modeled 25-yr trends during 21 st century –40 100-yr projections → –Mean 0.5° –>2.0° in only 3% of cases –Max 2.75° –(Celeste Johanson, Univ. of Washington)

30 Temperature deviation (GISS) versus latitude

31 Number of tropical pixels versus time for longitude -80 to -60 28 to 32 latitude 48 to 52 latitude 38 to 42 latitude 58 to 62 latitude

32 Number of tropical pixels for 58 to 62 latitude vs longitude

Download ppt "Lesson 2 AOSC 621. Radiative equilibrium Where S is the solar constant. The earth reflects some of this radiation. Let the albedo be ρ, then the energy."

Similar presentations

Ads by Google