2. Meridional atmospheric structure; heat and water transport. Recall that the most primitive equilibrium climate model can be written

Size: px
Start display at page:

Download "2. Meridional atmospheric structure; heat and water transport. Recall that the most primitive equilibrium climate model can be written"

Transcription

1 2. Meridional atmospheric structure; heat and water transport The equator-to-pole temperature difference DT was stronger during the last glacial maximum, with polar temperatures down by at least twice as much as equatorial ones compared to the present day. Some paleoclimate evidence also suggests that DT has been weaker in the past than today, including high-latitude incidence of temperate flora and fauna (50-70 MY) and low-latitude glaciations ( MY, ~2GY?). Temperature gradients are connected to energy transport via conservation laws, as well as winds on Earth due to its rotation. Today s surface temperature ranges from ~27C at the equator to ~-30C (on average) at the poles (see Fig. 1) Energy balance models Recall that the most primitive equilibrium climate model can be written (S/4)(1-A) = est S 4, (1) where S is the solar constant (1365 W/m 2 today), A is the planetary albedo (about 30% today), s is the Stefan-Boltzmann constant, T S the mean surface temperature (about 288K today), and e is an effective emissivity for earth (about 0.61 today) that decreases as atmospheric infrared opacity increases, due to the lower temperature as one goes up in the atmosphere (which produces Earth s greenhouse effect). We could write this as a function of latitude f: (S(f)/4)(1-A(f)) = e(f)st S (f) 4 + H(f) (2) where we have to add a transport term H(f) because energy can accumulate at certain latitudes due to transport by the atmosphere or ocean. Specifically, H µ - F where F is the horizontal flux of moist static energy carried within the atmosphere, ocean, and solid earth. We can calculate S(f) and observe A(f) and e(f) accurately from space today; if we plug these into (2), neglect H, and solve for an equilibrium T S (f), we find an equatorto-pole temperature gradient about twice as big as currently observed. That means that F is directed from warm to cold regions (as expected) and carries enough energy to reduce today s meridional gradient of T S to half the radiative equilibrium value. Directly observing F is difficult; current estimates are that between 1/4 and 1/3 is carried in the oceans, the rest in the atmosphere (virtually none in the solid earth). Today s atmospheric component is split about 50/50 between dry static energy (F 1 ) and latent heat (water vapor) transport (F 2 ), though this would change in different climates. A question central to climate change is how F(f) depends on T S (f). No definitive general theory has yet been developed, but GCM simulations can be used as a guide to behavior. Simple scaling arguments suggest that F 1 ~ (DT) 2, which would tend to prevent significant changes in DT. F 1 (f) probably also depends on other things like orography.

2 Even without a stabilizing dependence of F on DT, climate responses to global changes in S, A or e would according to (2) be similar at all latitudes. You need latitudinally varying changes in these parameters to change DT, and the more sensitive F is to DT, the larger these need to be. A at high latitudes should depend on ice cover; since ice should grow with decreasing T, this leads to a positive feedback that can produce polar amplification, or greater T changes at high latitudes than at low latitudes. Cloud cover can potentially change e and A in latitudinally varying ways, but no theories exist to predict this quantitatively. The latent heat flux F 2 depends on the amount of water vapor in the atmosphere. As temperatures increase, water vapor content increases at 6-13%/C, which will tend to drive F 2 higher with higher global T regardless of DT. This is another important source of polar amplification, which becomes more important in warmer climates (where the icealbedo feedback becomes inoperative) but less important in colder climates. The thermal wind balance and zonal winds Observations from the last glacial maximum (LGM) indicate stronger winds at mid latitudes. This is consistent with larger DT, according to a relationship known as the thermal wind balance. The average air flow over long time scales (days) above the surface is approximately in geostrophic balance. This means that the Coriolis force (which points to the right/left in the northern/southern hemisphere) opposes the force due to pressure gradients in the atmosphere. With little net force, the air cruises along on a path with gentle (average) curvature. The pressure gradients are caused by temperature gradients. With warm tropics (positive DT), pressure decreases more slowly with height (due to the reduced density of warm air) than at high latitudes. This leads to a pressure surplus in the tropics at higher levels, which pushes air toward the poles. Steady state occurs when the air begins moving eastward fast enough for the Coriolis force to counteract this push. Larger DT requires stronger flow; a faster rotation rate requires weaker flow. Winds near the surface are more complicated, since friction enters in to slow down the winds and provide a third force. The net result is that wind is nearly geostrophic, but blows toward low surface pressure. That tends to equalize surface pressures compared to what one finds aloft. The combined result at the surface is relatively weak winds that do not obey thermal wind balance. However, it appears that in midlatitudes upper-level winds basically pull the surface air along but at a slower speed, so that surface winds should be at least qualitatively related to DT aloft. Also, geostrophic balance is close enough so that you can tell the winds pretty well by looking at a sea-level pressure chart. The mean winds in the troposphere and stratosphere are dominated by the midlatitude jets, which peak near 10 km and decrease toward the surface (see fig. 2). The jets are strongest at the edge of the tropics because the Coriolis force is weakest near the equator (requiring stronger winds to generate the same force). In the tropics the temperature

3 gradients break down and become very small, leading to decreased winds. Close to the equator, Coriolis forces vanish and geostrophic balance itself no longer applies. Surface pressure maps reflect the strong mid-latitude westerlies (means blowing from the west), by indicating low pressure poleward and high pressure in the subtropics (see Fig. 3). The low pressure is concentrated in two centers in the northern hemisphere, known as the Aleutian and Icelandic lows. In the southern hemisphere there is a zonal strip of very low pressure near the border of Antarctica. In the tropics there are surface easterlies ( trade winds ). Poleward of the jets, winds are generally weaker and can be either direction. The thermal wind balance is also relevant to the polar night jet, a wind that circumnavigates the winter stratospheric polar vortex. This becomes stronger when the vortex is colder. Cold temperatures lead to ozone-destroying clouds. In the northern hemisphere, variability from the troposphere disturbs the polar night jet, limiting ozone destruction. Mechanisms of meridional energy transport In a completely thermal-wind balanced atmosphere, the winds would all be zonal and there would be no meridional energy transport. In reality, eddies occur which transport heat. In the tropics, there is a big, overturning eddy called the Hadley circulation (see Figure 5). Air rises in the summer hemisphere near the equator and sinks in the winter subtropics, carrying moist static energy into the winter hemisphere. The Hadley circulation exists because of the weak Coriolis force near the equator. Beyond 25 degrees latitude, the Hadley circulation abruptly gives way to a mainly zonal circulation. The net overturning circulation outside the Hadley circulation is weak and unimportant. Further poleward transport occurs in transient, quasi-horizontal eddies (transient means their wind averages to zero over time). These eddies tilt upward away from the equator, owing to the steep slope of the isentropic (constant potential temperature) surfaces (Figure 5). This is because air will conserve potential temperature when adiabatically moved to a different pressure. This upward slope means that air in the upper troposphere communicates with the tropical, near-surface atmosphere, not only in the tropics itself (via deep convection) but at all latitudes (via transient eddies). In the tropics, lapse rates are (thought to be) controlled purely by local thermodynamics, but at high latitudes they may be altered by low-latitude temperature changes via eddy transport (for example, a warmer tropics would tend to warm the mid-troposphere at mid-latitudes, making the lapse rate less negative). All of this applies particularly to the winter hemisphere; the summer hemisphere behaves a bit more like the tropics. Atmospheric energy balance and radiation The atmosphere is always losing infrared radiation to space. It must be heated by transport from the surface, which is mostly released as condensational heating (conversion of latent heat in water vapor). This is proportional to rainfall. Thus, Earth s

4 hydrologic cycle is controlled largely by atmospheric radiative cooling. A warmer atmosphere tends to cool faster, leading to more global rainfall (an alternative way to think of this is that with a highly absorbing greenhouse atmosphere, more of the radiation to space, which is the same according to eq. (1), comes from the atmosphere). In a very cold climate, condensational heating would eventually no longer dominate the atmospheric heat budget, which would decouple the hydrological cycle from atmospheric radiation. Water vapor is currently the strongest greenhouse gas in Earth s atmosphere. Normally, a warmer object radiates more energy. However, water vapor concentrations increase with T. Consequently, in the (saturated) absorbing bands of water vapor, the emission to space depends only on relative humidity rather than temperature. This makes climate more sensitive, and can even lead to a runaway greenhouse if water vapor concentrations become sufficient to saturate enough of water vapor s vibration-rotation spectrum (this is related to the Kombayashi-Ingersoll limit discussed by Pierrehumbert (2002) and may have occurred on Venus).

5 Figure 1

6 Figure 2

7 Figure 3

8 Figure 4

9 \ Figure 5

F = ma. ATS 150 Global Climate Change Winds and Weather. Scott Denning CSU CMMAP 1. Please read Chapter 6 from Archer Textbook

F = ma. ATS 150 Global Climate Change Winds and Weather. Scott Denning CSU CMMAP 1. Please read Chapter 6 from Archer Textbook Winds and Weather Please read Chapter 6 from Archer Textbook Circulation of the atmosphere and oceans are driven by energy imbalances Energy Imbalances What Makes the Wind Blow? Three real forces (gravity,

More information

General Atmospheric Circulation

General Atmospheric Circulation General Atmospheric Circulation Take away Concepts and Ideas Global circulation: The mean meridional (N-S) circulation Trade winds and westerlies The Jet Stream Earth s climate zones Monsoonal climate

More information

Interhemispheric climate connections: What can the atmosphere do?

Interhemispheric climate connections: What can the atmosphere do? Interhemispheric climate connections: What can the atmosphere do? Raymond T. Pierrehumbert The University of Chicago 1 Uncertain feedbacks plague estimates of climate sensitivity 2 Water Vapor Models agree

More information

warmest (coldest) temperatures at summer heat dispersed upward by vertical motion Prof. Jin-Yi Yu ESS200A heated by solar radiation at the base

warmest (coldest) temperatures at summer heat dispersed upward by vertical motion Prof. Jin-Yi Yu ESS200A heated by solar radiation at the base Pole Eq Lecture 3: ATMOSPHERE (Outline) JS JP Hadley Cell Ferrel Cell Polar Cell (driven by eddies) L H L H Basic Structures and Dynamics General Circulation in the Troposphere General Circulation in the

More information

The Planetary Circulation System

The Planetary Circulation System 12 The Planetary Circulation System Learning Goals After studying this chapter, students should be able to: 1. describe and account for the global patterns of pressure, wind patterns and ocean currents

More information

Wind: Global Systems Chapter 10

Wind: Global Systems Chapter 10 Wind: Global Systems Chapter 10 General Circulation of the Atmosphere General circulation of the atmosphere describes average wind patterns and is useful for understanding climate Over the earth, incoming

More information

ATMO 436a. The General Circulation. Redacted version from my NATS lectures because Wallace and Hobbs virtually ignores it

ATMO 436a. The General Circulation. Redacted version from my NATS lectures because Wallace and Hobbs virtually ignores it ATMO 436a The General Circulation Redacted version from my NATS lectures because Wallace and Hobbs virtually ignores it Scales of Atmospheric Motion vs. Lifespan The general circulation Atmospheric oscillations

More information

Atmospheric circulation

Atmospheric circulation Atmospheric circulation Trade winds http://science.nasa.gov/science-news/science-at-nasa/2002/10apr_hawaii/ Atmosphere (noun) the envelope of gases (air) surrounding the earth or another planet Dry air:

More information

General Circulation. Nili Harnik DEES, Lamont-Doherty Earth Observatory

General Circulation. Nili Harnik DEES, Lamont-Doherty Earth Observatory General Circulation Nili Harnik DEES, Lamont-Doherty Earth Observatory nili@ldeo.columbia.edu Latitudinal Radiation Imbalance The annual mean, averaged around latitude circles, of the balance between the

More information

Lecture 9: Climate Sensitivity and Feedback Mechanisms

Lecture 9: Climate Sensitivity and Feedback Mechanisms Lecture 9: Climate Sensitivity and Feedback Mechanisms Basic radiative feedbacks (Plank, Water Vapor, Lapse-Rate Feedbacks) Ice albedo & Vegetation-Climate feedback Cloud feedback Biogeochemical feedbacks

More information

Lecture 5: Atmospheric General Circulation and Climate

Lecture 5: Atmospheric General Circulation and Climate Lecture 5: Atmospheric General Circulation and Climate Geostrophic balance Zonal-mean circulation Transients and eddies Meridional energy transport Moist static energy Angular momentum balance Atmosphere

More information

1 Climatological balances of heat, mass, and angular momentum (and the role of eddies)

1 Climatological balances of heat, mass, and angular momentum (and the role of eddies) 1 Climatological balances of heat, mass, and angular momentum (and the role of eddies) We saw that the middle atmospheric temperature structure (which, through thermal wind balance, determines the mean

More information

Answer Key for Practice Test #2

Answer Key for Practice Test #2 Answer Key for Practice Test #2 Section 1. Multiple-choice questions. Choose the one alternative that best completes the statement or answers the question. Mark your choice on the optical scan sheet. 1.

More information

CHAPTER 4. THE HADLEY CIRCULATION 59 smaller than that in midlatitudes. This is illustrated in Fig. 4.2 which shows the departures from zonal symmetry

CHAPTER 4. THE HADLEY CIRCULATION 59 smaller than that in midlatitudes. This is illustrated in Fig. 4.2 which shows the departures from zonal symmetry Chapter 4 THE HADLEY CIRCULATION The early work on the mean meridional circulation of the tropics was motivated by observations of the trade winds. Halley (1686) and Hadley (1735) concluded that the trade

More information

CLIMATE AND CLIMATE CHANGE MIDTERM EXAM ATM S 211 FEB 9TH 2012 V1

CLIMATE AND CLIMATE CHANGE MIDTERM EXAM ATM S 211 FEB 9TH 2012 V1 CLIMATE AND CLIMATE CHANGE MIDTERM EXAM ATM S 211 FEB 9TH 2012 V1 Name: Student ID: Please answer the following questions on your Scantron Multiple Choice [1 point each] (1) The gases that contribute to

More information

CHAPTER 2 - ATMOSPHERIC CIRCULATION & AIR/SEA INTERACTION

CHAPTER 2 - ATMOSPHERIC CIRCULATION & AIR/SEA INTERACTION Chapter 2 - pg. 1 CHAPTER 2 - ATMOSPHERIC CIRCULATION & AIR/SEA INTERACTION The atmosphere is driven by the variations of solar heating with latitude. The heat is transferred to the air by direct absorption

More information

GEO1010 tirsdag

GEO1010 tirsdag GEO1010 tirsdag 31.08.2010 Jørn Kristiansen; jornk@met.no I dag: Først litt repetisjon Stråling (kap. 4) Atmosfærens sirkulasjon (kap. 6) Latitudinal Geographic Zones Figure 1.12 jkl TØRR ATMOSFÆRE Temperature

More information

Presentation A simple model of multiple climate regimes

Presentation A simple model of multiple climate regimes A simple model of multiple climate regimes Kerry Emanuel March 21, 2012 Overview 1. Introduction 2. Essential Climate Feedback Processes Ocean s Thermohaline Circulation, Large-Scale Circulation of the

More information

Chapter 9 External Energy Fuels Weather and Climate

Chapter 9 External Energy Fuels Weather and Climate Natural Disasters Tenth Edition Chapter 9 External Energy Fuels Weather and Climate Copyright The McGraw-Hill Companies, Inc. Permission required for reproduction or display. 9-1 Weather Versus Climate

More information

Radiative-Convective Models. The Hydrological Cycle Hadley Circulation. Manabe and Strickler (1964) Course Notes chapter 5.1

Radiative-Convective Models. The Hydrological Cycle Hadley Circulation. Manabe and Strickler (1964) Course Notes chapter 5.1 Climate Modeling Lecture 8 Radiative-Convective Models Manabe and Strickler (1964) Course Notes chapter 5.1 The Hydrological Cycle Hadley Circulation Prepare for Mid-Term (Friday 9 am) Review Course Notes

More information

Transient and Eddy. Transient/Eddy Flux. Flux Components. Lecture 3: Weather/Disturbance. Transient: deviations from time mean Time Mean

Transient and Eddy. Transient/Eddy Flux. Flux Components. Lecture 3: Weather/Disturbance. Transient: deviations from time mean Time Mean Lecture 3: Weather/Disturbance Transients and Eddies Climate Roles Mid-Latitude Cyclones Tropical Hurricanes Mid-Ocean Eddies Transient and Eddy Transient: deviations from time mean Time Mean Eddy: deviations

More information

Electromagnetic Radiation. Radiation and the Planetary Energy Balance. Electromagnetic Spectrum of the Sun

Electromagnetic Radiation. Radiation and the Planetary Energy Balance. Electromagnetic Spectrum of the Sun Radiation and the Planetary Energy Balance Electromagnetic Radiation Solar radiation warms the planet Conversion of solar energy at the surface Absorption and emission by the atmosphere The greenhouse

More information

COURSE CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION

COURSE CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION COURSE CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION DATE 4 JUNE 2014 LEADER CHRIS BRIERLEY Course Outline 1. Current climate 2. Changing climate 3. Future climate change 4. Consequences 5. Human

More information

Part-8c Circulation (Cont)

Part-8c Circulation (Cont) Part-8c Circulation (Cont) Global Circulation Means of Transfering Heat Easterlies /Westerlies Polar Front Planetary Waves Gravity Waves Mars Circulation Giant Planet Atmospheres Zones and Belts Global

More information

K32: The Structure of the Earth s Atmosphere

K32: The Structure of the Earth s Atmosphere K32: The Structure of the Earth s Atmosphere Chemical composition Vertical Layers Temperature structure Coriolis Force and horizontal structure Hadley Cells and Heat sources Current Molecular Composition

More information

Divergence, Spin, and Tilt. Convergence and Divergence. Midlatitude Cyclones. Large-Scale Setting

Divergence, Spin, and Tilt. Convergence and Divergence. Midlatitude Cyclones. Large-Scale Setting Midlatitude Cyclones Equator-to-pole temperature gradient tilts pressure surfaces and produces westerly jets in midlatitudes Waves in the jet induce divergence and convergence aloft, leading to surface

More information

DEAPS Activity 3 Weather systems and the general circulation of the atmosphere

DEAPS Activity 3 Weather systems and the general circulation of the atmosphere DEAPS Activity 3 Weather systems and the general circulation of the atmosphere Lodovica Illari 1 Introduction What is responsible for stormy weather? What causes relatively warm temperatures one day and

More information

Course Outline CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION. 1. Current climate. 2. Changing climate. 3. Future climate change

Course Outline CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION. 1. Current climate. 2. Changing climate. 3. Future climate change COURSE CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION DATE 4 JUNE 2014 LEADER CHRIS BRIERLEY Course Outline 1. Current climate 2. Changing climate 3. Future climate change 4. Consequences 5. Human

More information

Dynamics and Kinematics

Dynamics and Kinematics Geophysics Fluid Dynamics () Syllabus Course Time Lectures: Tu, Th 09:30-10:50 Discussion: 3315 Croul Hall Text Book J. R. Holton, "An introduction to Dynamic Meteorology", Academic Press (Ch. 1, 2, 3,

More information

Introduction to Climate ~ Part I ~

Introduction to Climate ~ Part I ~ 2015/11/16 TCC Seminar JMA Introduction to Climate ~ Part I ~ Shuhei MAEDA (MRI/JMA) Climate Research Department Meteorological Research Institute (MRI/JMA) 1 Outline of the lecture 1. Climate System (

More information

CHAPTER 6 Air-Sea Interaction Pearson Education, Inc.

CHAPTER 6 Air-Sea Interaction Pearson Education, Inc. CHAPTER 6 Air-Sea Interaction Chapter Overview The atmosphere and the ocean are one independent system. Earth has seasons because of the tilt on its axis. There are three major wind belts in each hemisphere.

More information

ATMS 321: Sci. of Climate Final Examination Study Guide Page 1 of 4

ATMS 321: Sci. of Climate Final Examination Study Guide Page 1 of 4 ATMS 321: Sci. of Climate Final Examination Study Guide Page 1 of 4 Atmospheric Sciences 321: Final Examination Study Guide The final examination will consist of similar questions Science of Climate Multiple

More information

The Structure and Motion of the Atmosphere OCEA 101

The Structure and Motion of the Atmosphere OCEA 101 The Structure and Motion of the Atmosphere OCEA 101 Why should you care? - the atmosphere is the primary driving force for the ocean circulation. - the atmosphere controls geographical variations in ocean

More information

Lecture 11: Meridonal structure of the atmosphere

Lecture 11: Meridonal structure of the atmosphere Lecture 11: Meridonal structure of the atmosphere September 28, 2003 1 Meridional structure of the atmosphere In previous lectures we have focussed on the vertical structure of the atmosphere. Today, we

More information

Climate and the Atmosphere

Climate and the Atmosphere Climate and Biomes Climate Objectives: Understand how weather is affected by: 1. Variations in the amount of incoming solar radiation 2. The earth s annual path around the sun 3. The earth s daily rotation

More information

Lecture 10: Climate Sensitivity and Feedback

Lecture 10: Climate Sensitivity and Feedback Lecture 10: Climate Sensitivity and Feedback Human Activities Climate Sensitivity Climate Feedback 1 Climate Sensitivity and Feedback (from Earth s Climate: Past and Future) 2 Definition and Mathematic

More information

Transient/Eddy Flux. Transient and Eddy. Flux Components. Lecture 7: Disturbance (Outline) Why transients/eddies matter to zonal and time means?

Transient/Eddy Flux. Transient and Eddy. Flux Components. Lecture 7: Disturbance (Outline) Why transients/eddies matter to zonal and time means? Lecture 7: Disturbance (Outline) Transients and Eddies Climate Roles Mid-Latitude Cyclones Tropical Hurricanes Mid-Ocean Eddies (From Weather & Climate) Flux Components (1) (2) (3) Three components contribute

More information

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds. What is an atmosphere? Planetary Atmospheres

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds. What is an atmosphere? Planetary Atmospheres Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds What is an atmosphere? Planetary Atmospheres Pressure Composition Greenhouse effect Atmospheric structure Color of the sky 1 Atmospheres

More information

Introduction to Atmospheric Circulation

Introduction to Atmospheric Circulation Introduction to Atmospheric Circulation Start rotating table Cloud Fraction Dice Results from http://eos.atmos.washington.edu/erbe/ from http://eos.atmos.washington.edu/erbe/ from http://eos.atmos.washington.edu/erbe/

More information

EART164: PLANETARY ATMOSPHERES

EART164: PLANETARY ATMOSPHERES EART164: PLANETARY ATMOSPHERES Francis Nimmo Last Week Radiative Transfer Black body radiation, Planck function, Wien s law Absorption, emission, opacity, optical depth Intensity, flux Radiative diffusion,

More information

Lecture 3: Global Energy Cycle

Lecture 3: Global Energy Cycle Lecture 3: Global Energy Cycle Planetary energy balance Greenhouse Effect Vertical energy balance Latitudinal energy balance Seasonal and diurnal cycles Solar Flux and Flux Density Solar Luminosity (L)

More information

Tropical Meridional Circulations: The Hadley Cell

Tropical Meridional Circulations: The Hadley Cell Tropical Meridional Circulations: The Hadley Cell Introduction Throughout much of the previous sections, we have alluded to but not fully described the mean meridional overturning circulation of the tropics

More information

Geophysics Fluid Dynamics (ESS228)

Geophysics Fluid Dynamics (ESS228) Geophysics Fluid Dynamics (ESS228) Course Time Lectures: Tu, Th 09:30-10:50 Discussion: 3315 Croul Hall Text Book J. R. Holton, "An introduction to Dynamic Meteorology", Academic Press (Ch. 1, 2, 3, 4,

More information

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds What is an atmosphere? 10.1 Atmospheric Basics Our goals for learning:! What is an atmosphere?! How does the greenhouse effect warm

More information

Atmospheric Circulation

Atmospheric Circulation Atmospheric Circulation Introductory Oceanography Instructor: Ray Rector Atmospheric Circulation Key Topics Composition and Structure Solar Heating and Convection The Coriolis Effect Global Wind Patterns

More information

ATMO 551a Fall The Carnot Cycle

ATMO 551a Fall The Carnot Cycle What is a arnot ycle and Why do we care The arnot ycle arnot was a French engineer who was trying to understand how to extract usable mechanical work from a heat engine, that is an engine where a gas or

More information

Winds and Global Circulation

Winds and Global Circulation Winds and Global Circulation Atmospheric Pressure Winds Global Wind and Pressure Patterns Oceans and Ocean Currents El Nino How is Energy Transported to its escape zones? Both atmospheric and ocean transport

More information

Space Atmospheric Gases. the two most common gases; found throughout all the layers a form of oxygen found in the stratosphere

Space Atmospheric Gases. the two most common gases; found throughout all the layers a form of oxygen found in the stratosphere Earth s atmospheric layers Earth s atmosphere is the layer of gases that surrounds the planet and makes conditions on Earth suitable for living things. Layers Earth s atmosphere is divided into several

More information

4. Atmospheric transport. Daniel J. Jacob, Atmospheric Chemistry, Harvard University, Spring 2017

4. Atmospheric transport. Daniel J. Jacob, Atmospheric Chemistry, Harvard University, Spring 2017 4. Atmospheric transport Daniel J. Jacob, Atmospheric Chemistry, Harvard University, Spring 2017 Forces in the atmosphere: Gravity g Pressure-gradient ap = ( 1/ ρ ) dp / dx for x-direction (also y, z directions)

More information

1. The vertical structure of the atmosphere. Temperature profile.

1. The vertical structure of the atmosphere. Temperature profile. Lecture 4. The structure of the atmosphere. Air in motion. Objectives: 1. The vertical structure of the atmosphere. Temperature profile. 2. Temperature in the lower atmosphere: dry adiabatic lapse rate.

More information

Clouds and Rain Unit (3 pts)

Clouds and Rain Unit (3 pts) Name: Section: Clouds and Rain Unit (Topic 8A-2) page 1 Clouds and Rain Unit (3 pts) As air rises, it cools due to the reduction in atmospheric pressure Air mainly consists of oxygen molecules and nitrogen

More information

2010 Pearson Education, Inc.

2010 Pearson Education, Inc. Chapter 10 Planetary Atmospheres: Mars, Venus, Earth What is an atmosphere? An atmosphere is a (usually very thin) layer of gas that surrounds a world. How does the greenhouse effect warm a planet? No

More information

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds

Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds Chapter 10 Planetary Atmospheres Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics Our goals for learning: What is an atmosphere? How does the greenhouse effect warm a planet? Why do atmospheric

More information

The general circulation: midlatitude storms

The general circulation: midlatitude storms The general circulation: midlatitude storms Motivation for this class Provide understanding basic motions of the atmosphere: Ability to diagnose individual weather systems, and predict how they will change

More information

The Transfer of Heat

The Transfer of Heat The Transfer of Heat Outcomes: S2-4-03 Explain effects of heat transfer within the atmosphere and hydrosphere on the development and movement of wind and ocean currents. Coriolis Effect In our ecology

More information

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds. What is an atmosphere? Earth s Atmosphere. Atmospheric Pressure

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds. What is an atmosphere? Earth s Atmosphere. Atmospheric Pressure Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics Our goals for learning What is an atmosphere? How does the greenhouse effect warm a planet? Why do atmospheric

More information

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics Our goals for learning What is an atmosphere? How does the greenhouse effect warm a planet? Why do atmospheric

More information

7 The General Circulation

7 The General Circulation 7 The General Circulation 7.1 The axisymmetric state At the beginning of the class, we discussed the nonlinear, inviscid, axisymmetric theory of the meridional structure of the atmosphere. The important

More information

Temperature (T) degrees Celsius ( o C) arbitrary scale from 0 o C at melting point of ice to 100 o C at boiling point of water Also (Kelvin, K) = o C

Temperature (T) degrees Celsius ( o C) arbitrary scale from 0 o C at melting point of ice to 100 o C at boiling point of water Also (Kelvin, K) = o C 1 2 3 4 Temperature (T) degrees Celsius ( o C) arbitrary scale from 0 o C at melting point of ice to 100 o C at boiling point of water Also (Kelvin, K) = o C plus 273.15 0 K is absolute zero, the minimum

More information

Ocean Mixing and Climate Change

Ocean Mixing and Climate Change Ocean Mixing and Climate Change Factors inducing seawater mixing Different densities Wind stirring Internal waves breaking Tidal Bottom topography Biogenic Mixing (??) In general, any motion favoring turbulent

More information

Topic # 12 How Climate Works

Topic # 12 How Climate Works Topic # 12 How Climate Works A Primer on How the Energy Balance Drives Atmospheric & Oceanic Circulation, Natural Climatic Processes pp 63-68 in Class Notes How do we get energy from this........ to drive

More information

Meteorology 311. General Circulation/Fronts Fall 2017

Meteorology 311. General Circulation/Fronts Fall 2017 Meteorology 311 General Circulation/Fronts Fall 2017 Precipitation Types Rain Snow growth of ice crystals through deposition, accretion, and aggregation. Freezing Rain Rain freezes when it hits the surface.

More information

10.1 TEMPERATURE, THERMAL ENERGY AND HEAT Name: Date: Block: (Reference: pp of BC Science 10)

10.1 TEMPERATURE, THERMAL ENERGY AND HEAT Name: Date: Block: (Reference: pp of BC Science 10) 10.1 TEMPERATURE, THERMAL ENERGY AND HEAT Name: Date: Block: (Reference: pp. 424-435 of BC Science 10) kinetic molecular theory: explains that matter is made up of tiny that are constantly. These atoms

More information

Weather Systems. Section

Weather Systems. Section Section 1 12.2 Objectives Compare and contrast the three major wind systems. Identify four types of fronts. Distinguish between highand low-pressure systems. Review Vocabulary convection: the transfer

More information

5.1. Weather, climate, and components of the climate system

5.1. Weather, climate, and components of the climate system 5. The climate system 5.1. Weather, climate, and components of the climate system The weather is characterized by the atmospheric conditions (e.g. temperature, precipitations, cloud cover, wind speed)

More information

Topic # 11 HOW CLIMATE WORKS PART II

Topic # 11 HOW CLIMATE WORKS PART II Topic # 11 HOW CLIMATE WORKS PART II The next chapter in the story: How differences in INSOLATION between low and high latitudes drive atmospheric circulation! pp 64 in Class Notes THE RADIATION BALANCE

More information

Unit 3 Review Guide: Atmosphere

Unit 3 Review Guide: Atmosphere Unit 3 Review Guide: Atmosphere Atmosphere: A thin layer of gases that forms a protective covering around the Earth. Photosynthesis: Process where plants take in carbon dioxide and release oxygen. Trace

More information

Topic # 11 HOW CLIMATE WORKS continued (Part II) pp in Class Notes

Topic # 11 HOW CLIMATE WORKS continued (Part II) pp in Class Notes Topic # 11 HOW CLIMATE WORKS continued (Part II) pp 61-67 in Class Notes To drive the circulation, the initial source of energy is from the Sun: Not to scale! EARTH- SUN Relationships 4 Things to Know

More information

Atmosphere, Ocean and Climate Dynamics Answers to Chapter 8

Atmosphere, Ocean and Climate Dynamics Answers to Chapter 8 Atmosphere, Ocean and Climate Dynamics Answers to Chapter 8 1. Consider a zonally symmetric circulation (i.e., one with no longitudinal variations) in the atmosphere. In the inviscid upper troposphere,

More information

Lesson Overview. Climate. Lesson Overview. 4.1 Climate

Lesson Overview. Climate. Lesson Overview. 4.1 Climate Lesson Overview 4.1 THINK ABOUT IT When you think about climate, you might think of dramatic headlines: Hurricane Katrina floods New Orleans! or Drought parches the Southeast! But big storms and seasonal

More information

Atmospheric Sciences 321. Science of Climate. Lecture 13: Surface Energy Balance Chapter 4

Atmospheric Sciences 321. Science of Climate. Lecture 13: Surface Energy Balance Chapter 4 Atmospheric Sciences 321 Science of Climate Lecture 13: Surface Energy Balance Chapter 4 Community Business Check the assignments HW #4 due Wednesday Quiz #2 Wednesday Mid Term is Wednesday May 6 Practice

More information

Boundary layer equilibrium [2005] over tropical oceans

Boundary layer equilibrium [2005] over tropical oceans Boundary layer equilibrium [2005] over tropical oceans Alan K. Betts [akbetts@aol.com] Based on: Betts, A.K., 1997: Trade Cumulus: Observations and Modeling. Chapter 4 (pp 99-126) in The Physics and Parameterization

More information

Introduction to Isentropic Coordinates:! a new view of mean meridional & eddy circulations" Cristiana Stan

Introduction to Isentropic Coordinates:! a new view of mean meridional & eddy circulations Cristiana Stan Introduction to Isentropic Coordinates:! a new view of mean meridional & eddy circulations" Cristiana Stan School and Conference on the General Circulation of the Atmosphere and Oceans: a Modern Perspective!

More information

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds Pearson Education, Inc.

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds Pearson Education, Inc. Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics Our goals for learning: What is an atmosphere? How does the greenhouse effect warm a planet? Why do atmospheric

More information

Week: Dates: 3/2 3/20 Unit: Climate

Week: Dates: 3/2 3/20 Unit: Climate clementaged.weebly.com Name: EVEN Period: Week: 28 30 Dates: 3/2 3/20 Unit: Climate Monday Tuesday Wednesday Thursday Friday 2 O 3 E *Vocabulary *Water in the Atmosphere and Clouds Notes *Cloud Drawings

More information

Environmental Science Chapter 13 Atmosphere and Climate Change Review

Environmental Science Chapter 13 Atmosphere and Climate Change Review Environmental Science Chapter 13 Atmosphere and Climate Change Review Multiple Choice Identify the choice that best completes the statement or answers the question. 1. Climate in a region is a. the long-term,

More information

Chapter 2. Heating Earth's Surface & Atmosphere

Chapter 2. Heating Earth's Surface & Atmosphere Chapter 2 Heating Earth's Surface & Atmosphere Topics Earth-Sun Relationships Energy, Heat and Temperature Mechanisms of Heat Transfer What happens to Incoming Solar Radiation? Radiation Emitted by the

More information

Planetary Atmospheres: Earth and the Other Terrestrial Worlds Pearson Education, Inc.

Planetary Atmospheres: Earth and the Other Terrestrial Worlds Pearson Education, Inc. Planetary Atmospheres: Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics Our goals for learning: What is an atmosphere? How does the greenhouse effect warm a planet? Why do atmospheric properties

More information

The Cosmic Perspective Planetary Atmospheres: Earth and the Other Terrestrial Worlds

The Cosmic Perspective Planetary Atmospheres: Earth and the Other Terrestrial Worlds Chapter 10 Lecture The Cosmic Perspective Seventh Edition Planetary Atmospheres: Earth and the Other Terrestrial Worlds Planetary Atmospheres: Earth and the Other Terrestrial Worlds 10.1 Atmospheric Basics

More information

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds. What is an atmosphere? About 10 km thick

Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds. What is an atmosphere? About 10 km thick Chapter 10 Planetary Atmospheres: Earth and the Other Terrestrial Worlds What is an atmosphere? Sources of Gas Losses of Gas Thermal Escape Earth s Atmosphere About 10 km thick Consists mostly of molecular

More information

Description of the Climate System and Its Components

Description of the Climate System and Its Components 1 Description of the Climate System and Its Components Outline This first chapter describes the main components of the climate system as well as some processes that will be necessary to understand the

More information

Course Outline. About Me. Today s Outline CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION. 1. Current climate. 2.

Course Outline. About Me. Today s Outline CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION. 1. Current climate. 2. Course Outline 1. Current climate 2. Changing climate 3. Future climate change 4. Consequences COURSE CLIMATE SCIENCE A SHORT COURSE AT THE ROYAL INSTITUTION DATE 4 JUNE 2014 LEADER 5. Human impacts 6.

More information

Topic # 12 Natural Climate Processes

Topic # 12 Natural Climate Processes Topic # 12 Natural Climate Processes A Primer on How the Energy Balance Drives Atmospheric & Oceanic Circulation, Natural Climatic Processes pp 63-68 in Class Notes RADIATION / ENERGY BALANCE Radiation

More information

Temperature Pressure Wind Moisture

Temperature Pressure Wind Moisture Chapter 1: Properties of Atmosphere Temperature Pressure Wind Moisture Thickness of the Atmosphere (from Meteorology Today) 90% 70% The thickness of the atmosphere is only about 2% of Earth s thickness

More information

ATMOSPHERE PACKET CHAPTER 22 PAGES Section 1 page 546

ATMOSPHERE PACKET CHAPTER 22 PAGES Section 1 page 546 Name: Period: ATMOSPHERE PACKET CHAPTER 22 PAGES 546-564 Section 1 page 546 1. Identify five main components of the atmosphere 2. Explain the cause of atmospheric pressure. 3. Why is atmospheric pressure

More information

Atmospheric Sciences 321. Science of Climate. Lecture 20: More Ocean: Chapter 7

Atmospheric Sciences 321. Science of Climate. Lecture 20: More Ocean: Chapter 7 Atmospheric Sciences 321 Science of Climate Lecture 20: More Ocean: Chapter 7 Community Business Quiz discussion Next Topic will be Chapter 8, Natural Climate variability in the instrumental record. Homework

More information

Climate vs. Weather. Weather: Short term state of the atmosphere. Climate: The average weather conditions in an area over a long period of time

Climate vs. Weather. Weather: Short term state of the atmosphere. Climate: The average weather conditions in an area over a long period of time Weather and Climate Climate vs. Weather Weather: Short term state of the atmosphere. Temperature, humidity, cloud cover, precipitation, winds, visibility, air pressure, air pollution, etc Climate: The

More information

The linear additivity of the forcings' responses in the energy and water cycles. Nathalie Schaller, Jan Cermak, Reto Knutti and Martin Wild

The linear additivity of the forcings' responses in the energy and water cycles. Nathalie Schaller, Jan Cermak, Reto Knutti and Martin Wild The linear additivity of the forcings' responses in the energy and water cycles Nathalie Schaller, Jan Cermak, Reto Knutti and Martin Wild WCRP OSP, Denver, 27th October 2011 1 Motivation How will precipitation

More information

Match (one-to-one) the following (1 5) from the list (A E) below.

Match (one-to-one) the following (1 5) from the list (A E) below. GEO 302C EXAM 1 Spring 2009 Name UID You may not refer to any other materials during the exam. For each question (except otherwise explicitly stated), select the best answer for that question. Read all

More information

Isentropic flows and monsoonal circulations

Isentropic flows and monsoonal circulations Isentropic flows and monsoonal circulations Olivier Pauluis (NYU) Monsoons- Past, Present and future May 20th, 2015 Caltech, Pasadena Outline Introduction Global monsoon in isentropic coordinates Dry ventilation

More information

ATS 421/521. Climate Modeling. Spring 2015

ATS 421/521. Climate Modeling. Spring 2015 ATS 421/521 Climate Modeling Spring 2015 Lecture 9 Hadley Circulation (Held and Hou, 1980) General Circulation Models (tetbook chapter 3.2.3; course notes chapter 5.3) The Primitive Equations (tetbook

More information

Assessment Schedule 2017 Earth and Space Science: Demonstrate understanding of processes in the atmosphere system (91414)

Assessment Schedule 2017 Earth and Space Science: Demonstrate understanding of processes in the atmosphere system (91414) NCEA Level 3 Earth and Space Science (91414) 2017 page 1 of 6 Assessment Schedule 2017 Earth and Space Science: Demonstrate understanding of processes in the atmosphere system (91414) Evidence Statement

More information

p = ρrt p = ρr d = T( q v ) dp dz = ρg

p = ρrt p = ρr d = T( q v ) dp dz = ρg Chapter 1: Properties of the Atmosphere What are the major chemical components of the atmosphere? Atmospheric Layers and their major characteristics: Troposphere, Stratosphere Mesosphere, Thermosphere

More information

Climate Dynamics (PCC 587): Clouds and Feedbacks

Climate Dynamics (PCC 587): Clouds and Feedbacks Climate Dynamics (PCC 587): Clouds and Feedbacks D A R G A N M. W. F R I E R S O N U N I V E R S I T Y O F W A S H I N G T O N, D E P A R T M E N T O F A T M O S P H E R I C S C I E N C E S D A Y 7 : 1

More information

Unit Three Worksheet Meteorology/Oceanography 2 WS GE U3 2

Unit Three Worksheet Meteorology/Oceanography 2 WS GE U3 2 Unit Three Worksheet Meteorology/Oceanography 2 WS GE U3 2 Name Period Section 17.3 1. 2. 3. 4. 5. 6. 7. 8. Of the following, which is NOT a factor that controls temperature? (C) latitude (D) longitude

More information

Key Feedbacks in the Climate System

Key Feedbacks in the Climate System Key Feedbacks in the Climate System With a Focus on Climate Sensitivity SOLAS Summer School 12 th of August 2009 Thomas Schneider von Deimling, Potsdam Institute for Climate Impact Research Why do Climate

More information

ESS 111 Climate & Global Change. Week 1 Weather vs Climate Structure of the Atmosphere Global Wind Belts

ESS 111 Climate & Global Change. Week 1 Weather vs Climate Structure of the Atmosphere Global Wind Belts ESS 111 Climate & Global Change Week 1 Weather vs Climate Structure of the Atmosphere Global Wind Belts Weather is the state of the atmosphere at a given place and time. For example, right now, the temperature

More information

Climate. Energy & Wind Masses. Ocean Explorer Module 5

Climate. Energy & Wind Masses. Ocean Explorer Module 5 Marine Science Lesson Enhancements based on Grade 11 & 12 curriculum in Physics, Chemistry & Biology Climate Energy & Wind Masses Ocean Explorer Module 5 Copyright 2017 Climate part 1 Page! 1 of! 14 Overview

More information

WEATHER. Review Note Cards

WEATHER. Review Note Cards WEATHER Review Note Cards Thermometer Weather instrument that measures air temperature Units include F, C, and K ESRT 13 Sling Psychrometer Weather instrument that measures relative humidity and dewpoint

More information

Weather Notes. Chapter 16, 17, & 18

Weather Notes. Chapter 16, 17, & 18 Weather Notes Chapter 16, 17, & 18 Weather Weather is the condition of the Earth s atmosphere at a particular place and time Weather It is the movement of energy through the atmosphere Energy comes from

More information