The State of the Atmosphere 1.Atmospheric mass and pressure 2.Temperature structure 3.Geopotential 4.Circulation 5.Water in the atmosphere.

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Alan Robock Department of Environmental Sciences Rutgers University, New Brunswick, New Jersey USA

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Presentation transcript:

The State of the Atmosphere 1.Atmospheric mass and pressure 2.Temperature structure 3.Geopotential 4.Circulation 5.Water in the atmosphere

Atmospheric mass and pressure From the equation of continuity, after integration for a polar cap limited by  In the long-term mean: Assuming that the atmosphere is a ideal gas (p=  RT) in hydrostatic equilibrium we have and by integrating: We can then rewrite the first equation as:(1)

The rapid decrease of density with height distinguishes the atmosphere from the ocean

Distribution of mass in terms of pressure

If H_surf=2.56x10 14 m 2 P North_h =983.6mb, P South_h =988.0mb, P Globe =983.6mb g=9.8 m/s 2 Then m_ North_h =2.57x10 18 kg m_ Souh_h =2.58x10 18 kg m_ Globe =5.15x10 18 kg...Distribution of mass in terms of pressure

The interhemispheric transport From Eq. (1) we can calculate the transport trough the equator: If  p=1mb/month

Global distribution of temperature

Vertical and meridional change

Temporal variability of temperature

Geopotential heights

Mean circulation

Correlation coefficient between northern hemisphere stratospheric geopotential at 50hPa and an index representing the tropospheric 500hPA NAO.

Hadley model Hadley (1735) wanted to explain trade wind circulation Complements of E. Kant and J. Dalton Ferel (1856): Coriolis force and Geostrophic wind Helmholtz: the role of friction-deviation of wind includes turbulent viscosity for the first time

Actual vertical circulation

Kinetic energy of the atmosphere K=K TE +K SE +K M K=0.5[u 2 m +v 2 m ] K TE =0.5[(u‘ 2 +v‘ 2 ) m ] K SE =0.5[u m *2 +v m *2 ] K M =0.5([u m ] 2 +[v m ] 2 )

Precipitation