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Chapter 5: Atmospheric Structure and Energy Balance (I) Characteristics of the Atmosphere Thickness, air pressure, density Air pressure and density decrease with altitude 90% of its mass (5.1 x 1018 kg) is within 16 km (10 mi) of the surface (about 0.0025 times the radius of the Earth) 97% of air in first 29 km or 18 mi; 99% 32 km (18 mi); 99.9% 47km (30mi) Atmospheric motions can therefore be considered to occur “at” the Earth’s surface The greatest and most important variations in its composition involve water in its various phases Water vapor Clouds of liquid water Clouds of ice crystals Rain, snow and hail Composition of the Atmosphere Dry Air TRACE GASES Argon (.93%) and Carbon Dioxide (.03%) Ozone (.000004%) Solid particles (dust, sea salt, pollution) also exist Water vapor is constantly being added and subtracted from the atmosphere, and varies from near 0% (deserts) to 3-4% (warm, tropical oceans and jungles) Vertical Structure of the Atmosphere 4 distinct layers determined by the change of temperature with height Extends to 10 km in the extratropics, 16 km in the tropics Contains 80-90% of the atmospheric mass, and 50% is contained in the lowest 5 km (3.5 miles) It is defined as a layer of temperature decrease The total temperature change with altitude is about 72°C (130°F), or 6.5°C per km (lapse rate) • It is the region where all weather occurs, and it is kept well stirred by rising and descending air currents • The transition region of no temperature change is the “tropopause”: it marks the beginning of the next layer Vertical Structure of the Atmosphere 4 distinct layers determined by the change of temperature with height Extends to about 50 km It is defined as a layer of temperature increase and is stable with very little vertical air motion – a good place to fly! Why does temperature increase? The major heating is the UV of sunlight absorbed by O3.. When the sunlight travel down, the UV will become less and less available, so the temperature increase with height… • The transition region to the next layer is the “stratopause” Atm. vertical structure • Air pressure p at sea level is 1 atm. = 1.013 bar = 1013 mb • p decr. with altitude by factor of 10 every 16 km. • T decr. with altitude in troposphere, rises in stratosphere drops in mesosph. rises in thermosph. Temperature (II) Radiation Energy Objectives: • Electromagnetic (EM) radiation & spectrum • Energy flux • Blackbody radiation -- Wien’s Law & Stefan-Boltzmann Law • Planetary energy balance UNBC EM radiation wavelength later t • EM radiation includes visible light, ultraviolet, infrared, microwaves. • wavelength • period T, frequency = 1/T • wave speed or phase speed c = /T = • Speed of light in vacuum: c = 3.00108 m/s UNBC •c = /T => = cT = c/ longer period waves => longer ? wavelength UNBC Energy flux • Power = energy per unit time (watt W = J/s) • Flux F = power per unit area (W/m2) less flux high lat. => less F UNBC EM spectrum • EM radiation classified by their wavelength or freq. UNBC Inverse-square law • Solar flux S falls off as r0 S S 0 r 2 e.g. if r = 2r0 => S = S0/4 S UNBC Blackbody radiation • Absolute temperature in degrees Kelvin (K) • 0 K = -273°C (coldest possible T) • All bodies emit EM radiation • e.g. humans emit mainly infrared (IR) • “Blackbody” emits (or absorbs) EM rad. with 100% efficiency. UNBC Wien’s Law Planck function (blackbody rad. curve) max = const./T Rad. flux Temp. T in K const. = 2898 m max refers to the Wavelength of energy radiated with greatest intensity. max wavelength UNBC Blackbody rad. curves for Sun & Earth max = const./T Temp. T in K const. = 2898 m UNBC Stefan-Boltzmann Law Planck function (blackbody rad. curve) F = T4 Rad. flux = 5.67 x 10-8 W/m2/K4 total F = area under curve wavelength UNBC Planetary energy balance • Earth is at steady state: Energy emitted by Earth = Energy absorbed • E emitted = (area of Earth) Te4 = 4 Re2 Te4 ..(1) (Te= Earth’s effective rad. temp., Re= Earth’s radius) • E absorbed = E intercepted - E reflected • Solar E intercepted = S Re2 (solar flux S) • Solar E reflected = AS Re2 (albedo A) • E absorbed = (1-A) S Re2 • (1) => 4 Re2 Te4 = (1-A) S Re2 UNBC Magnitude of greenhouse effect • Te4 = (1-A) S/4 • Te = [(1-A) S/(4 )]1/4 (i.e. fourth root) • Te = 255K = -18°C, very cold! • Observ. mean surf. temp. Ts = 288K = 15°C • Earth’s atm. acts as greenhouse, trapping outgoing rad. • Ts - Te = Tg, the greenhouse effect • Tg = 33°C UNBC Greenhouse effect of a 1-layer atm. •Energy balance at Earth’s surface: Ts4 = (1-A)S/4 + Te4 ..(1) •Energy balance for atm.: Ts4 = 2 Te4 .. (2) S/4 Te AS/4 Te4 Atm. (1-A)S/4 Ts Ts4 Earth UNBC Te4 Subst. (2) into (1): Te4 = (1-A)S/4 ..(3) (same eq. as in last lec.) Divide (2) by ; take 4th root: Ts = 21/4 Te = 1.19 Te For Te = 255K, Ts = 303K. (Observ. Ts = 288K) Tg = Ts - Te = 48K, 15K higher than actual value. • Overestimation: atm. is not perfectly absorbing all IR rad. from Earth’s surface. UNBC (III) Modelling Energy Balance Objectives: • Effects of clouds • Earth’s global energy budget • Climate modelling • Climate feedbacks UNBC Cumulus Cumulonimbus Stratus Cirrus UNBC Climatic effects of clouds • Without clouds, Earths’ albedo drops from 0.3 to 0.1. By reflecting solar rad., clouds cool Earth. • But clouds absorb IR radiation from Earth’s surface (greenhouse effect) => warms Earth. • Cirrus clouds: ice crystals let solar rad. thru, but absorbs IR rad. from Earth’s sfc. => warm Earth • Low level clouds (e.g. stratus): reflects solar rad. & absorbs IR => net cooling of Earth UNBC • IR rad. from clouds at T4 • High clouds has much lower T than low clouds => high clouds radiate much less to space than low clouds. => high clouds much stronger greenhouse effect. UNBC Earth’s global energy budget UNBC Climate Modelling •“General circulation models” (GCM): Divide atm./oc. into 3-D grids. Calc. variables (e.g. T, wind, water vapor, currents) at grid pts. => expensive. •e.g. used in double CO2 exp. GFDL, Princeton UNBC • Weather forecasting also uses atm. GCMs. Assimilate observ. data into model. Advance model into future => forecasts. • Simpler: 1-D (vertical direction) radiativeconvective model (RCM): Doubling atm. CO2 => +1.2°C in ave.sfc.T • Need to incorporate climate feedbacks: • water vapour feedback • snow & ice albedo feedback • IR flux/Temp. feedback • cloud feedback UNBC Water vapour feedback • If Ts incr., more evap. => more water vapour => more greenhouse gas => Ts incr. • If Ts decr., water vap. condenses out => less greenhouse gas => Ts decr. • Feedback factor f = 2. • From RCM: T0 = 1.2°C (without feedback) => Teq = f T0 = 2.4°C. Ts (+) Atm. H2O Greenhouse effect UNBC Snow & ice albedo feedback • If Ts incr. => less snow & ice => decr. planetary albedo => Ts incr. • As snow & ice are in mid-high lat. => can only incorp. this effect in 3-D or 2-D models, not in 1-D RCM. Ts (+) snow & ice cover planetary albedo UNBC IR flux/Temp. feedback • So far only +ve feedbacks => unstable. • Neg. feedback: If Ts incr. => more IR rad. from Earth’s sfc. => decr. Ts Ts (-) Outgoing IR flux •But this feedback loop can be overwhelmed if Ts is high & lots of water vap. around => water vap. blocks outgoing IR => runaway greenhouse (e.g. Venus) UNBC Uncertainties in cloud feedback • Incr. Ts => more evap. => more clouds • But clouds occur when air is ascending, not when air is descending. If area of ascending/descending air stays const. => area of cloud cover const. • High clouds or low clouds? High clouds warm while low clouds cool the Earth. • GCM’s resolution too coarse to resolve clouds => need to “parameterize” (ie. approx.) clouds. • GCM => incr. Ts => more cirrus clouds => warming => positive feedback. => Teq = 2 -5°C for CO2 doubling UNBC