Winds and Global Circulation
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2 Winds and Global Circulation Atmospheric Pressure Winds Global Wind and Pressure Patterns Oceans and Ocean Currents El Nino
3 How is Energy Transported to its escape zones? Both atmospheric and ocean transport are crucial Buoyancy-driven convection drives vertical transport Latent heat is at least as important as sensible heat
4 Atmospheric Circulation in a nutshell Hot air rises (rains a lot) in the tropics Air cools and sinks in the subtropics (deserts) Poleward-flow is deflected by the Coriolis force into westerly jet streams in the temperate zone Jet streams are unstable to small perturbations, leading to huge eddies (storms and fronts) that finish the job
5 Atmospheric Pressure As the atmosphere is held down by gravity, it exerts a force upon every surface (pressure = force per unit area) At sea level the force is the weight of 1 kg of air that lies above each square centimeter of the surface (around 15 lbs per in 2 ) Figure 5.1, p. 151
6 atmospheric pressure decreases rapidly with altitude near the surface Therefore a small change in elevation will often produce a significant change in air pressure Figure 5.4, p. 154
7 Two columns of air same temperature same distribution of mass 500 mb level 1000 mb 1000 mb
8 Cool the left column; warm the right column The heated column expands The cooled column contracts 500 mb original 500 mb level 500 mb 1000 mb 1000 mb
9 The level of the 500 mb surface changes; the surface pressure remains unchanged The level corresponding to 500 mb is displaced downward in the cooler column original 500 mb level The 500 mb surface displaced upward in t warmer column new 500 mb level in warm air new 500 mb level in cold air The surface pressure remains the same since both columns still contain the same mass of air mb 1000 mb
10 A pressure difference in the horizontal direction develops above the surface The 500 mb surface is displaced downward in the cooler column original 500 mb level Low High The 500 mb surface displaced upward in t warmer column new 500 mb level in warm air new 500 mb level in cold air 1000 mb 1000 mb The surface pressure remains the same since both columns still contain the same mass of air.
11 Air moves from high to low pressure in the middle of the column, causing the surface pressure to change. original 500 mb level Low High 1003 mb 997 mb
12 Air moves from high to low pressure at the surface Where would we have rising motion? original 500 mb level Low High High Low 1003 mb 997 mb
13 What have we just observed? Starting with a uniform atmosphere at rest, we introduced differential heating The differential heating caused different rates of expansion in the fluid The differing rates of expansion resulted in pressure differences along a horizontal surface. The pressure differences then induced flow in the fluid This is a microcosm of how the atmosphere converts heating into motions
14 Surface Pressure Maps Altitude-adjusted surface station pressures are used to construct sea level pressure contours
15 Differences in air pressure = a pressure gradient The pressure gradient forces acts at right angles to the isobars (90 degrees) weak pressure gradient strong pressure gradient
16 high pressure low pressure pressure gradient force v geostrophic winds
17 Gradient Wind
18 Geostrophic Wind The Geostrophic wind is flow in a straight line in which the pressure gradient force balances the Coriolis force. 994 mb Lower Pressure 996 mb 998 mb Higher Pressure Note: Geostrophic flow is often a good approximation high in the atmosphere (>500 meters)
19 High pressure (anticyclone) Side View From above H L H L L air descends surrounding air is relatively low
20 Low pressure (depressions, cyclone) From above Side View L H L H H air ascends surrounding air is relatively high
21 Friction forces as wind flows over the surface friction reduces the speed friction also changes the direction of the geostrophic wind the pressure gradient force over powers the Coriolis effect as a result wind flow across the isobars
22 H L Northern Hemisphere anticyclone cyclone Southern Hemisphere H L
23 90 o N 60 o N Cold High Pressure But heat is transported from the Equator to the Poles - how? 30 o N 0 o Warm Low Pressure SUN 30 o S 60 o S 90 o N Earth
24 Fig. 7-6, p. 151
25 How is Energy Transported to its escape zones? Both atmospheric and ocean transport are crucial Buoyancy-driven convection drives vertical transport Latent heat is at least as important as sensible heat
26 What a single cell convection model would look like for a non-rotating earth Thermal convection leads to formation of convection cell in each hemisphere Energy transported from equator toward poles What would prevailing wind direction be over N. America with this flow pattern on a rotating earth?
27 What s wrong with the 1-cell model? Neglects effect of rotation - with rotation, winds would cause earth to spin down - with rotation, the upper level winds would accelerate to unphysical speeds near the pole.
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29 Coriolis Force acts to the right in the Northern Hemisphere hysics
30 Coriolis Effect The Coriolis Effect deflects moving objects to the right in the northern hemisphere and to the left in
31 General Circulation of the Earth s Atmosphere 90 o N 60 o N 30 o N 0 o 30 o S 60 o S 90 o N Deflection No Deflection Deflection Deflection is least at the equator and greatest at the poles
32 Fig. 7-12, p. 154
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34 Wind patterns on a rotating Earth 3 circulation cells in each hemisphere
35 Key features of three cell model Hadley cell (thermally direct cell) - driven by meridional gradient in heating - air rises near equator and descends near 30 degrees - explains deserts; trade winds; ITCZ Ferrel Cell (indirect thermal cell) - driven by heat transports of eddies - air rises near 60 degrees and descends near 30 degrees - explains surface westerlies from Weak winds found near Equator (doldrums) 30 degrees (horse latitudes) Boundary between cold polar air and mid-latitude warmer air is the polar front
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39 90 o N 60 o N 30 o N 0 o L warm air rises at the equator producing low pressure (Intertropical Convergence Zone, ITCZ) and flows towards the poles 30 o S 60 o S 90 o N
40 90 o N 60 o N 30 o N 0 o 30 o S 60 o S H L H Cold air sinks at 30 o N and S latitude Creating high pressure (subtropical high pressure, STH) 90 o N
41 90 o N 60 o N 30 o N 0 o 30 o S 60 o S 90 o N H Northeasterly and southeasterly surface winds flow from the subtropical high pressure belts (30 o N and S) to the low pressure belt (ITCZ) at the equator (calm winds: doldrums) L H westerly surface winds flow from the subtropical high pressure belts towards higher latitudes
42 90 o N 60 o N 30 o N 0 o 30 o S L westerly surface winds are forced to rise around 60 o N and S latitude when they encounter cold polar easterly winds from the poles resulting in Subpolar Low pressure (SPL) belts H L H 90 o N 60 o S L
43 H 90 o N 60 o N 30 o N L H cold air sinks at the poles producing polar high (PH) pressure regions 0 o L 30 o S H 60 o S L 90 o N H
44 Figure 5.17, p. 163
45 H 90 o N 60 o N 30 o N 0 o 30 o S 60 o S 90 o N H L H L H L polar jet stream polar jet stream subtropical jet streams Jet streams are streams of fast moving air aloft that occur where atmospheric temperature gradients are strong
46 Temperature Patterns Stronger seasonal heating and cooling on land produces asymmetry Poleward distortion of isotherms over northern high latitude oceans Equatorward distortion over subtropics
47 Seasonal Migration of ITCZ Mean position is somewhat north of Equator Strong departures from zonal mean position driven by seasonal heating over land (Especially over Asia, S. America, Africa)
48 Monsoons In January high pressure over the land produces dry winds Air is flowing towards the ITCZ Figure 5.20, p. 167
49 Monsoons In July the position of the ITCZ moves North low pressure over the land causes winds to flow off the ocean this brings heavy rainfall Figure 5.20, p. 167
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51 Polar Front Jet Stream Polar front jet stream forms along polar front where strong thermal gradient causes a strong pressure gradient Strong pressure gradient force and coriolis force produce strong west wind parallel to contour lines Polar jet sometimes splits into north and south branches
52 Fast air currents, 1000 s of km s long, a few hundred km wide, a few km thick Typically find two jet streams (subtropical and polar front) at tropopause in NH When would you expect the jets to be strongest? Jet Streams
53 Smooth westward flow of upper air westerlies Develop at the polar front, and form convoluted waves eventually pinch off Primary mechanism for poleward heat transfere Pools of cool air create areas of low pressure Rossby Waves Figure 5.26, p. 171
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55 The dishpan experiment A tank of water with a hot equator and a cold pole is rotated Troughs, ridges and eddies are produced, similar to patterns observed in earth s general circulation
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57
58 movies
59 The Earth s Oceans Ocean currents produced by: 1) winds 2) density differences in sea water 3) Coriolis force 4) shape of ocean basins 5) astronomical factors (TIDES)
60 Ocean Currents driven mostly by wind blowing over the surface however, currents move slowly wind lag behind wind speed so often called drifts
61 Ocean currents large continuously moving loops (gyres) produced by winds, Coriolis force and land masses Figure 5.32, p. 175
62 Fig. 8-2, p. 172
63 Each hemisphere contains a tropical and subtropical gyre N. Subtropical Gyre North Tropical Gyre South Tropical Gyre EQUATOR S. Subtropical Gyre
64 Surface Currents redistribute heat
65 Upwelling where cold water rises from deep ocean areas and where the Coriolis forces prompts ocean currents to diverge from coastlines Figure 5.37, p. 180
66 Deep-sea currents driven by differences in temperature and salinity much slower than surface currents Figure 5.32, p. 180
67 The Ocean Conveyor Belt Deep-sea currents driven by differences in temperature and salinity much bigger and slower than surface currents
68 El Niño Southern Oscillation (ENSO) Trade winds promote cold water upwelling in eastern tropical Pacific Cool, deep water is nutrient rich and supports rich ecosystem (plankton, fish, birds, ) Weaker trades lead to weaker upwelling. Warm nutrient-poor tropical water replaces the cold, nutrient-rich water. called El Niño (boy child) Every few years this El Niño (surface warming) persists and is widespread Huge ecosystem and economic losses Alters weather patterns over much of the world El Niño 0-1 La Niña
69 Sea Surface Temperatures ( o C) El Niño Normal La Niña La Niña: cold surface water moves over central and eastern Pacific.
70 El Niño Sea Surface Temperature Anomalies o C Normal La Niña
71 Normal conditions equatorial Pacific
72 ENSO (El Nino - Southern Oscillation) conditions
73 Animations on the web Idealized ENSO wave For animation of most recent anomaly asee
74 Why do we care about ENSO? Global impacts on weather. Long timescale (months) yields improved seasonal prediction. Provides insight into coupled behavior of oceans and atmosphere may lead to better overall understanding of climate
75 Weather Variation: ENSO cycle winter summer
76 Impacts of El Niño Droughts Fires Agricultural productivity Water supply Extreme Precipitation Floods Erosion Disease Transportation Impacts through marine food chain Natural ecological responses Economic
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