1 / 21

METO 637

METO 637. Lesson 1. Fig. 1.14. Tropopause. Stratopause. Mesopause. 1. Troposphere- literally means region where air “turns over” -temperature usually decreases (on average ~6.5 °C/km) with altitude. 2. Stratosphere- layer above the tropopause, little mixing occurs in

chill
Télécharger la présentation

METO 637

An Image/Link below is provided (as is) to download presentation Download Policy: Content on the Website is provided to you AS IS for your information and personal use and may not be sold / licensed / shared on other websites without getting consent from its author. Content is provided to you AS IS for your information and personal use only. Download presentation by click this link. While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server. During download, if you can't get a presentation, the file might be deleted by the publisher.

E N D

Presentation Transcript

  1. METO 637 Lesson 1

  2. Fig. 1.14

  3. Tropopause Stratopause Mesopause 1. Troposphere- literally means region where air “turns over” -temperature usually decreases (on average ~6.5°C/km) with altitude 2. Stratosphere- layer above the tropopause, little mixing occurs in the stratosphere, unlike the troposphere, where “turbulent mixing” is common 3. Mesosphere- defined as the region where temperature again decreases with height. 4. Thermosphere- region with very little of the atmosphere’s mass. high energy radiation received by the thermosphere (high temperatures experienced). A small density of molecules (not much “heat” would be felt).

  4. HYDROSTATIC EQUATION Where H is called the atmospheric scale height

  5. HYDROSTATIC EQUATION-2

  6. HYDROSTATIC EQUATION-3 If we assume that g, T, and M* are constant then we get the equations H is called the scale height

  7. Atmospheric Pressure • Pressure at a point is the weight of air above that point • A column of air at the surface weighs about 1 kilogram per square cm. • Ideal gas law PV = nRT • However the atmosphere also contains water vapor which can condense at certain temperatures. In this case the ideal gas law does not hold

  8. Fig. 1.12

  9. Adiabatic Lapse Rate • The First Law of Thermodynamics can be expressed as: dU = dq + dw where dU is the change in internal energy, dq is the heat supplied to the system, and dw is the is the work done on the system. • dH, the change in enthalpy, can be written as dH = dU + pdV + Vdp • When we raise a parcel of air there is no heat input, hence dq=0 (adiabatic) and dw=pdV • Therefore dH = -Vdp

  10. Adiabatic Lapse Rate • The heat capacity of a gas at constant pressure, Cp, is defined as (dH/dT) so that Cp dT= Vdp • From the hydrostatic equation we get dp = -g σ dz • Hence Cp dT = -V g σ dz • For a unit mass of gas V=1/σ and we get

  11. Adiabatic Lapse Rate • For Venus, Earth, Mars and Jupiter the calculated values of Γd are 10.7, 9.8, 4.5 and 20.2 K per kilometer. • The dry adiabatic lapse rate plays an important role in atmospheric stability.

  12. Fig. 3.17

  13. Lapse Rates and Stability • Lapse rate is the rate at which the real atmosphere falls off with altitude – the environmental lapse rate • An average value is 6.5 ºC per kilometer • This should be compared with the adiabatic lapse rate of 10 ºC. • If the environmental lapse rate is less than 10 ºC, then the atmosphere is absolutely stable • If greater than 10 ºC, it is absolutely unstable

  14. Wet adiabatic lapse rate • The presence of condensable vapors, such as water vapor, complicates the process. • As the parcel of air ascends it cools at the dry adiabatic lapse rate until the water vapor reaches saturation – then condensation takes place. • This releases latent heat – which can raise the temperature of the air parcel. • Now the lapse rate depends on the amount of water vapor – wet adiabatic lapse rate.

  15. Role of atmospheric stability Temperature inversions produce very stable atmospheric conditions in which mixing is greatly reduced. There are two general types of inversions: surface inversions and inversions aloft. Surface inversions are the result of differential radiative properties of the Earth’s surface and the air above. The Earth is a much better absorber and radiator of energy than air; thus, in the late morning and afternoon hours the lower atmosphere is unstable. The opposite is true in the evening; a stable atmosphere with little vertical mixing prevails.

  16. The Nocturnal Inversion • On clear nights, a temperature inversion develops near the surface. - Air temperature usually decreases with height. An inversion is a layer of air where temperature increases with height. - Because the layer of air in the inversion is warmer than the air below it, the cooler air below the inversion cannot rise above it. Pollutants near the surface are therefore trapped below the inversion in the overnight hours.

  17. Fig. 3.18

  18. Role of Atmospheric Stability Inversions aloft are associated with prolonged, severe pollution episodes. These types of inversions are caused by the sinking air associated with the center of high pressure systems (subsidence). As the air sinks it is warmed adiabatically. Turbulence at the very lowest part of the atmosphere prevents subsidence from warming that portion of the atmosphere. Los Angles pollution episodes as well as those over the Mid-Atlantic region are the result of inversions aloft associated with strong high pressure systems.

  19. Temperature Inversions

  20. Composition of the Earth’s Troposphere H2 PM O2 CH4 N2 CO N2O O3 ←SO2, NO2, CFC’s, etc Ar CO2 Inert gases

  21. Atmospheric composition

More Related