1. Climate: What we know about it, How we know about it, and What we’re doing to it.]

2. CO 2 and the Greenhouse Effect CO2 concentrations between 1995 and 1990

3. CO2 concentrations in ice cores 1000 to 2000 AD

4. global view: CO2 concentrations 1000 to 2000 AD. Note change during industrial revolution!

5. Global Antarctica

7. How the Greenhouse effect works 1. Different frequencies of light act differently 2.Greenhouse Gasses in Earth’s atmosphere trap infrared light (heat) Same process that makes your car warm on a cold winter day, or heats up a Greenhouse!

8. Most of the radiant energy from the sun is concentrated in the visible and near-visible parts of the spectrum. The narrow band of visible light, between 400 and 700 nm, represents 43% of the total radiant energy emitted.

9. Water, Carbon Dioxide (CO2), Methane (CH4), Nitrous Oxide (N2O), Fuorocarbons (CFCs) What are the major Greenhouse Gasses?

10. Greenhouse Effect The rise in temperature that the Earth experiences because certain gases in the atmosphere trap energy from the sun. Without these gases, heat would escape back into space and Earth’s average temperature would be about 60ºF colder. Because of how they warm our planet, these gases are referred to as greenhouse gases. Gases include: water vapor, carbon dioxide, nitrous oxide, and methane Trace greenhouse gases are relatively transparent to incoming visible light from the sun, yet opaque to the energy radiated from the earth.

11. Northern Hemisphere Temperature since 1900 A.D.

13. Northern Hemisphere Temperature since 1400 A.D.

14. Temperature Carbon Dioxide

16. What does the future hold? What is “climate variability”? What is “interannual climate variability?” Why is it important? What can we learn about past climate? How are our activities impacting climate?

17. Climate varies on long (millennial) timescales

18. Climate varies on short (interannual) timescales

19. Why is understanding interannual variability important? 1) It is necessary if we are going to make a reasonable prediction of future climate.

20. Why is understanding interannual variability important? 2) It provides a framework for understanding variability in other systems.

21. The Pacific Decadal Oscillation Sea surface temperatures.

23. Time for a movie!

24. The isotope paleothermometer The  18 O isotope ratio in water is influenced by temperature – both during evaporation of H 2 O from the ocean and its eventual precipitation on land as rain or snow. At high latitudes, there is a very strong, approximately linear relationship between  18 O and local temperature.

25. What is “delta 18 O”? The ratio of 18 O/ 16 O in ice is compared to the ratio of 18 O/ 16 O in average ocean water. This comparison is called  18 O. Variations in the  18O of the oxygen in the water molecule, H2O, is used in climate studies

26. Why does  18 O relate to temperature? This equilibrium is temperature dependent The O 18 /O 16 ratio provides an accurate record of ancient water temperature.

29. Worldwide Ice Core Sites

31. Mt. Logan, Yukon (Canada)

32. What can we learn about interannual climate variability from ice cores?

33. Annual layers in glacier ice

34. Central England temperature estimates After Lamb, 1982 “Medieval warm period” “Little ice age”

35. Ice core data: trends removed r =+.52

36. Siple – 1400-1983

37. Siple Dome- 1900-1996

38. Abrupt Climate Change End of the “Younger Dryas” took <50 years

39. Instrumental data (thermometers!) “Proxy” data (tree rings, ice cores, corals)

40. Central Greenland temperatures 10-year average temperatures from the GISP2 ice core

41. Central Greenland  18 O

42. The GISP2 ice core record

43. Northern Hemisphere Temperature since 1400 A.D.

44. Ice coring sites Queen Maud Land Siple Dome Siple

45. Spatial covariance of Antarctic temperature with PC1

46. Antarctic T trends since 1982 AVHRR (infrared) satellite observations

47. Queen Maud Land Siple Dome Siple

48. What to do next? A good example is how Society dealt with the Ozone Hole

54. 1.UV radiation breaks off a chlorine atom from a CFC molecule. 2.The chlorine atom attacks an ozone molecule (03), breaking it apart and destroying the ozone. 3.The result is an ordinary oxygen molecule (0) and a chlorine monoxide molecule (ClO). 4.The chlorine monoxide molecule (ClO) is attacked by a free oxygen atom releasing the chlorine atom and forming an ordinary oxygen molecule (O). 5.The chlorine atom is now free to attack and destroy another ozone molecule (03). One chlorine atom can repeat this destructive cycle thousands of times.