SIT WITH YOUR GROUP TODAY TOPIC # 12 HOW CLIMATE WORKS

1. Tuesday Oct 26th SIT WITH YOUR GROUP TODAYTOPIC # 12 HOW CLIMATE WORKS I-3 IS DUE TODAY! Please deposit your I-3 WORKSHEET[STAPLED!] at the FRONT OF THE CLASSROOM according to GROUP # (NOTE: we will also accept Worksheets on Thursday if you don’t have yours today or need it to finish your write-up tonight.) The I-3 Write-Up is due in D2L Dropbox by 11:59 pm tonight. As soon as you come in today, get your GROUP FOLDER & finish up G-3 if your group is not quite done . . . .

2. RQ-6 is due on THURSDAY Oct 28th Warning: there is LOTS of reading for this one! TEST #3 is scheduled for a week from TODAY. . . . . The Top 10 List will be posted by Friday.

3. WRAP –UP of G-3 ASSIGNMENT Applying the Energy Balance Terms Your task is to decide which component or componentsworking togetherare most directly related to or responsible forthe observed phenomenon. # 1 – #12 : Left side of equation # 13 - #15: Right side of equation p 53

4. THE G-3 ANSWERS

5. 5. + together = the Greenhouse Effect 3. 2. 1. gases of atmosphere scatter shorter blue wavelengths 4. Noon: more & dusk: more The LEFT side of the equation:

6. 6. (dust, thicker atmosphere scatters longer red/orange wavelengths) 7. radiates day & night; camera senses IR 9. leads to distinct shadows, while diffuse SW radiation does not 8.

7. 10. All wavelengths of visible part of spectrum are scattered & transmitted in a colored spectrum by raindrops 12. More is absorbed, leads to more which can then warm up car 11. Attempt to increase absorption & reduce into eyes; reduces glare

8. LE H 14. Wet mud evaporates from pig & cools him: also heat from pig’s body is conducted into soil: 13. Hot air (less dense than surroundingcool air) rises in a convection current & lifts balloon G 15. June is hot & dry in Tucson. Dry, hot air can “hold” more water vapor, so water in cooler pads is evaporated easily. Hence more energy goes into instead of This cools the house! LE H The RIGHT Side of the Equation:

9. Topic # 12How Climate Works A “Primer” on How the Energy Balance Drives Atmospheric & Oceanic Circulation, Natural Climatic Processes pp 63-68 in Class Notes

10. How do we get energy from this . . . . . . . . to drive this ?

11. . . . . or this ? http://www.vets.ucar.edu/vg/T341/index.shtml

12. . . . .which leads to Global Climatic Regions: . . . .and CHANGES in these regions!

13. Hotter! Drier! Wetter! from Dire Predictions text

14. It all happens because of changes in the RADIATION / ENERGY BALANCE ! “Radiation Balance” part All components are referring to electromagnetic radiation All components are referring to modes of heat energy transfer or heat energy storage involving matter “Energy Balance” part

15. The is then able to be used in thermal energy “heat transfer” processes which manifest themselves as weather & climate! Start out here, with energy from the SUN radiated to Earth and so forth . . . “Radiation Balance” part = “Energy Balance” part

16. Thermal Energy Review Heat (def) = the thermal energy that is transferred from one body to another because of a temperature difference.  • Sensible Heat transfer (H) • Latent Heat transfer (LE)plus (after transfer) thermal energy can be STORED (G) Review

17. Ultimate source of energy is the SUN (SW) After absorption of SW, LW energy is radiated in & out by EARTH & Atmosphere Goes into the HEAT TRANSFER processes that drive WEATHER & CLIMATE ! Any NET (leftover) energy ENERGY IN THE EARTH-ATMOSPHERE SYSTEM

18. The Earth [as viewed from space] . . . has the organized, self-contained look of a live creature, full of information, marvelously skilled in handling the sun. ~ Lewis Thomas

19. LINKING THE ENERGY BALANCE TO ATMOSPHERIC CIRCULATION . . . We’ll start with the SUN (SOLAR INSOLATION) IN – SOL- ATION = Amount of incoming solar energy received by a point on Earth’s surface p 63

20. To drive the circulation, the initial source of energy is from the Sun: EARTH-SUN Relationships 4 Things to Know about Earth-Sun Relationships: Earth orbits Sun in one year Orbit is not a perfect circle ( = an ellipse ) Earth’s orbit around Sun can be “traced” on a plane (“Plane of the Ecliptic” – plane passes thru the center of Sun & Earth) Earth’s axis tilts 23.5  from a  to the “Plane of The Ecliptic” Not to scale! http://mesoscale.agron.iastate.edu/agron206/animations/01_EarthSun.html

21. These 4 Earth-Sun Properties lead to:the 2 factorsthat determine the AMOUNT OF SOLAR INSOLATION as the seasons progress: (1) INTENSITY of sun’s rays(perpendicular to surface = more intense) (2) DURATIONof daily insolation(longer day length = more insolation) p 63

22. Zenith point changes with latitude A useful term: ZENITH = The point directly overhead INTENSITY is greatest at any spot on Earth when sun is closest to the ZENITH! 

23. QUICKIE LATITUDE REVIEW: 90 N 66.5 N 23.5 N 0 23.5 S 66.5 S 90 S

24. EARTH-SUN RELATIONSHIPS & The SEASONS: VIEW THE ANIMATION:http://mesoscale.agron.iastate.edu/agron206/animations/01_EarthSun.html

25. JUNE SOLSTICE As viewed from one side of Sun

26. JUNE SOLSTICE As viewed from the other side of the Sun

27. JUNE SOLSTICE p 63

28. 24 hours of sunlight Most intense solar radiation JUNE SOLSTICE p 63

29. MARCH EQUINOX Equinox = “equal night” p 79

30. SEPTEMBER EQUINOXdifferent seasonal position in orbit . . . . . . but same latitudinal insolation as March Equinox

31. 12 hours of sunlight Most intense solar radiation MARCH & SEPTEMBER EQUINOXES p 63

32. DECEMBER SOLSTICE

33. 24 hours of darkness Most intense solar radiation DECEMBER SOLSTICE p 63

34. http://mesoscale.agron.iastate.edu/agron206/animations/01_EarthSun.htmlhttp://mesoscale.agron.iastate.edu/agron206/animations/01_EarthSun.html Recap

35. THE RADIATION BALANCE &THE GENERAL CIRCULATION OF THE ATMOSPHERE p 64

36. HOW IT ALL FITS TOGETHER: The amount of outgoing TERRESTRIAL LW / IR varies by latitude too -- Over the course of a year . . . The amount of INCOMING SW (Insolation) absorbed by EARTH varies by LATITUDE (MORE comes in near the Equator, less near the Poles) MORELW / IR is emitted at warmer LOW LATITUDES, LESS in cooler HIGH LATITUDES  LOW LATITUDES absorb MORE energy than HIGH LATITUDES HOWEVER . . . p 64

37. The EQUATOR-POLE DIFFERENCES of what goes OUT from the EARTH are less than the EQUATOR-POLE DIFFERENCES of what comes IN from the SUN p 64

38. BUT the amount of outgoing LW is only slightly different from latitude to latitude & Equator to Pole LESS SW coming in SW in < LW out MORE SW coming in SW in > LW out p 64

39. The result is a NET SURPLUS of energy in the low latitudes & a NET DEFICIT in the high latitudes p 64

40. POLE EQUATOR POLE Now lets look at a Pole to Pole Transect p 64

41. Net radiation deficit Net radiation deficit What do the black & gray areas represent? (at top of atmosphere) Net radiation surplus p 64

42. http://geography.uoregon.edu/envchange/clim_animations/

44. Global-scale air motions are driven by thermal differences: Northern Hemisphere Southern Hemisphere EQUATOR COLD POLAR REGIONS HOT TROPICS COLD POLAR REGIONS 

45. HOT TROPICS COLD POLAR REGIONS COLD POLAR REGIONS From SGC-I Chapter 4

46. cold polar air vs. warm low lat air sinking dry subtropical air rising tropical warm,moist air sinking dry subtropical air warm low lat airvs. cold polar air

47. LOW PRESSURE AREAS: Hot surface  Rising air expansion and cooling of air, and condensation of water vapor  clouds, and possibly precipitation . . . HUMID REGIONS 

48. How do H2O droplets in warm, tropical clouds coalesce and grow so that they become heavy enough to fall as rain in the ITCZ? 

49. Mini-Zombie Break !

50. DANCE YOUR PH.D! “Precipitation Initiation in Warm Clouds” This dances shows how a rain drop can form when one SLIGHTLY LARGER RAIN DROP is present among a population of smaller drops. In the tropics, really large drops (heavy enough to fall as rain ) only form after mixing occurs.