6Before you leave this section 1. Be able to list the 4 means of energy transfer, and identify the one which transfers all energy into and out of the Earth’s climate system.2. Be able to describe the means by which energy is transferred in each.3. Be able to reproduce, with explanation, four concept sketches of the energy transfer mechanisms.
7What controls the quantity and type of energy the Earth System receives? How much?What type?
14Before you leave this section 1. Name the laws and understand the physical concepts behind the control that the surface temperature of an object exerts on the quantity and dominant wavelength of Electromagnetic Radiation that it emits.2. Understand why these two properties of Electromagnetic Radiation are related in the opposite fashion to the temperature of the object.3. Be aware of what the term “temperature” of an object actually means in terms of energy and the various scales that we use to measure it.
18Before you leave this section 1. Graph the types and quantities of radiation being emitted by the Sun and Earth.2. Know the relative ordering of the various components of the Electro-magnetic Radiation spectrum based on wavelength, including the colors of the visible portions of that spectrum.
21Before you leave this section 1. Be able to describe conceptually the derivation of the Solar Constant.2. Know the numerical value of the Solar Constant and be able to provide a verbal definition.3. Explain why the Solar Constant may not actually be a true “constant”, but vary periodically with a frequency of about 11 years
22ZENITH ANGLE AND WHY SHOULD WE CARE? WHAT IS THEZENITH ANGLE AND WHY SHOULD WE CARE?
24Before you leave this section 1. Be able to define the zenith angle.2. Know what the zenith angle will be at sunrise and sunset and when it will at its minimum.3. Explain how the zenith angle controls the proportion of the Solar Constant falling on a unit area (square meter) of the Earth’s surface.
25Why are some places hot and others cold Why are some places hot and others cold? Why are some times of the year warmer than others?A. SPATIALB. TEMPORAL1. Annual2. Seasonal3. Daily
26CAN WE QUANTIFY THE EFFECT OF THE ZENITH ANGLE AND LATITUDE AT NOON?SUNNEquatorCenter ofEarthS
27CAN WE QUANTIFY THE EFFECT OF THE ZENITH ANGLE AND LATITUDE AT NOON?SUNNEquatorCenter ofEarthS
28CAN WE QUANTIFY THE EFFECT OF THE ZENITH ANGLE AND LATITUDE AT NOON?SUNNEquatorCenter ofEarthS
29CAN WE QUANTIFY THE EFFECT OF THE ZENITH ANGLE AND LATITUDE AT NOON?SUNNEquatorCenter ofEarthS
30Ten parallel rays representing the solar constant (345Wm-2) SUN
31Ten parallel rays representing the solar constant (345Wm-2) SUN
32Before you leave this section 1. Be able to sketch the relationship between the latitude of a locations and the zenith angle at noon on March and September 21.2. Be able to explain why the outside of the Earth’s atmosphere at various latitudes will receive varying portions of the solar constant at noon on these days.3. Understand the trigonometric way in which the zenith angle controls the proportion of the solar constant intercepted.4. Understand this trigonometric function sufficiently well to be able to explain why large/small zenith angles are associated with varying proportions of the solar constant.
33HOW DOES THE EARTH’S ORBIT AROUND THE SUN AFFECT INSOLATION? BYLTS
34Before you leave this section 1. Be able to identify the dates of the Aphelion and Perihelion.2. Know approximate Earth-Sun distances at these times, and the average Earth-Sun distance.3. Understand how to make the appropriate adjustment to the value of the solar constant based upon actual Earth-Sun distance, and be aware of the potential magnitude of this impact.
35S S U N U N s June 21 N Sun on horizon z = 90° Sun overhead z = 0° CancerEquatorUSun overhead z = 0°NAntarcticsSun on horizon z = 90°
36S S U N U N December 22 N s WHERE IS THE SUN OVERHEAD AT NOON? Sun on horizon z = 90°SUNSArcticZ = >0°= = 23.5°Sun overhead z = 0°UEquatorCapricornN23.5°SSun on horizon z = 90°s
37BOTTOM LINEMarch and September: Summer (Jun. in N, Dec. in S): Winter (Dec. in N, Jun. in S):
38Before you leave this section 1. Given the latitude of a location and the time of the year, be able to estimate the zenith angle at noon.2. Know at which latitude the sun will be directly overhead at the varying times of year.3. Know the latitudes beyond which the sun is never directly overhead.4. Know the latitudes beyond which there is at least one day of total darkness (and one of light) and the seasons in which these occur.
39Why do the lengths ofDay and Night vary with the seasons?September 21SUNJune 21December 21March 21
40s s s N N N Latitude Degrees North June Solstice Hours of Daylight Arctic C.CancerEquatorCapricornAntarctic C.sssLatitudeDegreesNorthJune SolsticeHours ofDaylightMarch/SeptemberEquinoxDecember Solstice906 months12hr0 hr804 months702 months66.524 hr5016 hr8 hr4015 hr9 hr3014 hr10 hr2013 hr11 hr1012.5hr11.5 hr12 hr
42Before you leave this section 1. Be able to sketch the orientation of the Earth’s axis of rotation with respect to the Sun during the course of the Earth’s annual revolution around the Sun, and identify the Circle of Illumination.2. Given key times of year and/or key geographic latitudes be able to estimate the length of daylight.3. Understand the 4 “bottom line” items with regard to controls on the seasonal and spatial variations in the length of daylight.
49Before you leave this section 1. Be able to integrate information concerning spatial and temporal scales of variability of insolation.2. Explain the significance of the Equator, Tropics and Arctic and Antarctic circles in terms of patterns of insolation.3. Sketch the temporal and spatial variability of insolation at the top of the Earth’s atmosphere , and therefore the basic input to the Earth’s climate system.
501. Atmospheric Composition. WHAT MAKES OUR ATMOSPHERE DISTINCT FROM SPACE?1. Atmospheric Composition.ALL ATMOSPHERE18.104.22.168.TRACE GASES22.214.171.124.
51WHAT MAKES OUR ATMOSPHERE DISTINCT FROM SPACE? 1. Density of Gases.
53Before you leave this section 1. Know the major chemical constituents of the Earth’s atmosphere and the trace gases which will be important in later discussions.2. Understand the vertical distribution of gases in the Earth’s atmosphere.3. Understand the concept of Atmospheric Pressure and how this varies vertically in the atmosphere.4. Know how Atmospheric Pressure is measured.
57THE EQUATION OF STATE FOR AN IDEAL GAS. PUTTING IT ALL TOGETHER! P = R. ρ. TP =R =ρ =T =
58PRACTICAL APPLICATION P = R. ρ. TNormal Lapse Rate:
59Before you leave this section 1. Name and understand the law relating the temperature of a gas and the volume that the gas occupies (at a fixed pressure).2. Name and understand the law relating the pressure on a gas and the volume that the gas occupies (at a fixed temperature).3. Be able to follow the linkages by which differences in the supply of insolation ultimately impact atmospheric pressures and movements within the atmosphere.4. Know the equation of state for an ideal gas and show how it encompasses both Charles’ and Boyle’s Law.5. Show how this determines the rate at which air cools and warms as it rises and falls respectively.
61Before you leave this section 1. Label in the correct vertical sequence, the four thermal layers within the atmosphere, and the boundaries that separate them.2. Identify those zones which display normal and reverse temperature gradients.3. Explain why those reverse gradients exist and the gases that are responsible for them.4. Be able to explain what is believed to cause the “hole in the ozone layer”, and why it might be of environmental concern.
62WHERE DOES THE INSOLATION GO TO? – SHORTWAVE RADIATION BUDGET
63Before you leave this section 1. Understand what is meant by scattering and its impact upon insolation.2. Identify the means by which energy is absorbed by the atmosphere.3. Understand the concept of albedo.4. Delineate the quantities of insolation effected by each atmospheric process.5. Determine the global average percentages of insolation returned to space, and those stored in the atmosphere and at the Earth’s surface.
66Before you leave this section 1. Have an understanding of the albedo of various naturally occurring surfaces.2. Explain the Pole – Equator differences in albedo.3. Explain differences in albedo of the Arctic and Antarctic.4. Identify global zones of rainforest and deserts by their albedo.
70Before you leave this section 1. Identify the three major sinks to which insolation gets sent in the Earth system, noting the major global ocean-atmosphere features to which these are linked.2. Understand why the same chemical compound (water) can occur in three very different natural states, and what it is about the behavior of that compound which determines the state.3. Understand the concept of Latent Heat and how it is stored/released from water in its three natural states without changing the temperature of the water.4. Know the quantities of energy required/released when water changes states between solid and liquid and liquid and gas – the latent heat of fusion and the latent heat of vaporization.
74What Would Temperatures be Without Greenhouse Gases? SUNEARTH WITH GREENHOUSEATMOSPHEREEARTH WITHOUTATMOSPHERE
75DO OTHER PLANETS HAVE GREENHOUSE EFFECTS? Just how smart are we in this class?PlanetSolarConstant,Wm-2PlanetaryAlbedo,%EffectiveRadiatingTemperatureKObservedSurfaceGreenhouseWarmingMars14715217(-56°C, -94°F)220 (-53°C, -87°F)3 (7°F)Earth34531255 (-18°C, - 9°F288 (15°C, 66°F)33 (73°FVenus65375232 (-41°C, -60°F)700 (427°C, 929°F)468 (989°F)
76Before you leave this section 1. Understand how greenhouse gases permit shortwave radiation to enter, but prevent long wave radiation from leaving, the atmosphere.2. Be aware the increases in some greenhouses in the atmosphere and the potential they may have for increasing the amount of energy stored in the Earth’s system, partly manifested by global temperatures.3. Be able to show the extent of the “Greenhouse Effect” naturally on Earth.
78Before you leave this section 1. Understand how energy is lost from the surface of the Earth to the atmosphere.2. Be able to explain why the atmosphere itself emits longwave radiation back to the surface of the Earth and to space.3. Explain why a change in the quantity of greenhouse gases (natural or anthropogenic) in the atmosphere will impact the quantities of direct outgoing longwave radiation and the temperature of the atmosphere before a new equilibrium between incoming and outgoing radiation to the Earth system can be established.
79NORTHERN HEMISPHERE MERIDIONAL RADIATION BALANCE AND TRANSFER0°~35°90°Latitude
80Before you leave this section 1. Describe and explain the meridional (latitudinal) distribution of annual insolation.2. Describe and explain the meridional (latitudinal) distribution of annual outgoing longwave radiation.3. Define global zones of surplus and deficit energy balance, and the approximate location of the boundary between the two.4. Derive the distribution of cumulative net poleward (meridional) transfer of energy across the surface of the globe required to balance out surplus and deficits.
81How is Energy Moved? P = R. ρ. T Tropopause North Pole 2 2 1 South
82Sir Edmund forgot The rotation of the Earth NorthPoleTropopauseSouthPole
85Before you leave this section 1. Describe the dominant three dimensional pattern of air circulation within the Earth’s atmosphere.2. Locate and account for the dominant patterns of surface atmospheric pressure belts on the globe.3. Identify the global pattern of surface pressure gradients down which the surface winds of the world will flow.
86CORIOLIS EFFECT Earth Rotating in anti-clockwise direction Lat. Circum. Velocity80° km km.hr-170° km km.hr-160° km km.hr-150° km 1078 km.hr-140° km 1284 km.hr-130° km 1450 km.hr-120° km 1574 km.hr-110° km 1648 km.hr-10° km 1670 km.hr-1Lat. Circum. VelocityAll latitudes rotate with the same ANGULAR VELOCITY (360°/24hrs)15°.hr-1.However LINEAR VELOCITIES change with latitude.
87VIEWED FROM ABOVE NORTH POLE Earth Rotating inanti-clockwise direction
88Merry-go-round is moving frame of reference Trees are fixed frame of reference
90CORIOLIS AS GEOGRAPHIC VARIABLE Rate of Change of Linear Velocity of Rotation400020003000100090°N80°N70°N60°N, Reykjavik50°N, Southampton40°N, Philadelphia30°N, Gainesville20°N, Guantanamo10°N, San José0°, Quito, Equator
92CORIOLIS GOES TRUCKING IN A FIXED FRAME OF REFERENCE, 104!VelocityDistance per unit timeAccelerationChange in Velocityper unit timeChange inVelocity+Distance-TimeTimet = 0
93CORIOLIS (CB) IN A MOVING FRAME OF REFERENCE!VelocityDistance per unit timeAccelerationChange in Velocityper unit time87Change inVelocity+Distance654TimeTime321t = 012345678
94CORIOLIS PUTS THE PEDAL TO THE METAL IN A MOVING FRAME OF REFERENCE! VelocityDistance per unit timeAccelerationChange in Velocityper unit time4Change inVelocity+Distance32TimeTime1t = 012345678
95Quantitative Expression CORIOLIS EFFECTQuantitative ExpressionCoriolis Effect proportional to:-2Ω . V. Sin (φ).where:Ω =V =Φ =
96Before you leave this section 1. Know Ferrel’s Law and the apparent direction in which moving objects are deflected from their intended paths in each hemisphere.2. Understand how (and why) the Coriolis effect varies as a function of latitude.3. Understand the relationship between the Coriolis effect and the linear velocity of the moving object.
99Before you leave this section 1. Be able to construct a diagram of global surface pressures and winds.2. Be able to designate the correct name to each set of planetary surface winds.3. Be able to explain why the degree of deflection from the pressure gradient force is greater in some regions of the world than others (and hence the slight variation in nomenclature procedure).
100CYCLONIC AND ANTICYCLONIC FLOWS Trust me I am a Doctor!CYCLONE (LOWN)ANTI-CYCLONENORTHERNSOUTHERN1) Pressure Gradient2) Coriolis EffectLH
101Before you leave this section 1. Be able to construct predicted air flows around low pressure (cyclones) and high pressure cells (anticyclones) in either hemisphere based simply upon considerations of pressure gradient and Coriolis effect.
102DIFFERENCES IN OCEANIC AND CONTINENTAL THERMAL PROPERTIES Differences in Specific Heat.Differences in Latent Heat Flux.Differences in the Penetration of Radiation.Differences in Mixing.
107Before you leave this section 1. Be able to explain the concept of Specific Heat and why Oceans and Continents possess such different values.2. Be able to explain why the partitioning of insolation over continents and oceans is different and the impact that this is likely to have on temperatures.3. Discuss the impact that varying depths to which insolation can penetrate soil/rock and water will impact the surface temperatures of both global surfaces.4. Explain the various mechanisms of mixing of surface ocean waters which may act to redistribute energy away from the ocean surface.
108CAN WE BRING THIS ALL TOGETHER TO EXPLAIN PATTERNS OF GLOBAL CLIMATE?Our tool kit:123456
119Before you leave this section 1. Be able to combine the elements of the class thus far to define annual average pressure belts and cells over the major ocean basins and continents of the world using a simple two-continent, one ocean models.2. Through the use of sketches be able to define the location and nature of major ocean currents (cold and warm) using the same simple model .3. Identify the major global exceptions to these generalizations, and be able to explain why and how they differ.
126Before you leave this section 1. With the aid of the simple concept sketches, describe and explain the physical reasoning for the shifts in boreal pressure belts and wind directions in the northern hemisphere summer.2. With the aid of the simple concept sketches, describe and explain the physical reasoning for the shifts in boreal pressure belts and wind directions in the northern hemisphere winter.
152Before you leave this section With the aid of the simple concept sketches, be able to describe and explain the physical reasoning for the following:1. The distribution of global precipitation, specifically the equatorial and mid-latitude precipitation belts.2. The role of topography in modifying global precipitation patterns.3. The distribution of global deserts.4. The role of surface ocean currents in modifying the global distribution of precipitation and deserts.