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Exploring Climate Models: From 0-D to 3-D Atmospheric Simulations

Dive into the complexity of climate models, from simple 0-D ideas to detailed 3-D simulations, exploring radiative transfer, water vapor, cloud dynamics, and feedback mechanisms. Understand the IPCC definitions of radiative forcing and the impact of gases, ozone, and aerosols on Earth's energy balance. Delve into the hierarchy of climate models and the challenges of estimating the effects of pollutants on vertical distribution.

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Exploring Climate Models: From 0-D to 3-D Atmospheric Simulations

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  1. PHY2505 - Lecture 19 1-D climate models

  2. Last lecture Review of Liou IPCC definitions of radiative forcing This lecture 1-D radiative-convective climate models IPCC results Final lecture Climate and planetary atmospheres Overview

  3. Hierarchy of models: simple ideas 0-D 1-D```````````````2-D 3-D Global mean Radiative- Energy GCM’s effective convective balance temperature Balance TOA…. at every……. Include……. Include Fs –FIR level N-S flow feedbacks Radiative transfer Equations of motion Equations for water vapor & cloud Thermodynamic equation

  4. Hierarchy of models 0-D 1-D```````````````2-D 3-D Global mean Radiative- Energy GCM’s effective convective balance temperature Radiative transfer Equations of motion Equations for water vapor & cloud Thermodynamic equation

  5. 1-D radiative-convective models Convection significantly reduces surface (& low level) temperature Radiative transfer Equations of motion Equations for water vapor & cloud Thermodynamic equation

  6. 1-D radiative-convective models CLEAR CLOUDY Radiative transfer Equations of motion Equations for water vapor & cloud Thermodynamic equation

  7. 1-D radiative-convective models Convective adjustment scheme: Radiative flux divergence due to convection Static stability From first law of thermodynamics, see Liou p467 Then local rate of change of temperature from : Equations for water vapor & cloud Thermodynamic equation

  8. IPCC results Equations for water vapor & cloud Thermodynamic equation

  9. IPCC results: well-mixed gases FRAD calculated according to RTE: FS-FIR IPCC results from 2001 differ from IPCC 1995, 1992 because of new HITRAN data base. Addition of thousands of lines cause change in forcing results of 1.5% for doubling of CO2, greater differences for less known species Equations for water vapor & cloud Thermodynamic equation

  10. IPCC results: well-mixed gases TOTAL FORCING: SAR: 2.45 +- 15% Wm-2 IPCC 2001: 2.43+-10%Wm-2 Doubling of CO2 ~ 3.7Wm-2 Equations for water vapor & cloud Thermodynamic equation

  11. IPCC results: ozone Highly variable: Stratospheric ozone loss causes a negative forcing: Cooling from stratosphere more important than increased solar transfer to surface: uncertainties due to difficulty in obtaining vertical profiles Equations for water vapor & cloud Thermodynamic equation

  12. IPCC results: ozone Highly variable: Tropospheric ozone increases causes a positive forcing: Difficulty estimating magnitude due to uncertainty of how pollution will effect vertical distribution Equations for water vapor & cloud Thermodynamic equation

  13. IPCC results: ozone Equations for water vapor & cloud Thermodynamic equation

  14. IPCC results: aerosols Direct effects: scattering and absorption Indirect: cloud Equations for water vapor & cloud Thermodynamic equation

  15. IPCC results: aerosols Equations for water vapor & cloud Thermodynamic equation

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