DOCSLIB.ORG

Oceanography 200, Spring 2008 Armbrust/Strickland Study Guide Exam 1

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Oceanography 200, Spring 2008 Armbrust/Strickland Study Guide Exam 1 Oceanography 200, Spring 2008 Armbrust/Strickland Study Guide Exam 1 Geography of Earth & Oceans Latitude & longitude Properties of Water Structure of water molecule: polarity, hydrogen bonds, effects on water as a solvent and on freezing Latent heat of fusion & vaporization & physical explanation Effects of latent heat on heat transport between ocean & atmosphere & within atmosphere Definition of density, density of ice vs. water Physical meaning of temperature & heat Heat capacity of water & why water requires a lot of heat gain or loss to change temperature Effects of heating & cooling on density of water, and physical explanation Difference in albedo of ice/snow vs. water, and effects on Earth temperature Properties of Seawater Definitions of salinity, conservative & non-conservative seawater constituents, density (sigma-t) Average ocean salinity & how it is measured 3 technology systems for monitoring ocean salinity and other properties 6 most abundant constituents of seawater & Principle of Constant Proportions Effects of freezing on seawater Effects of temperature & salinity on density, T-S diagram Processes that increase & decrease salinity & temperature and where they occur Generalized depth profiles of temperature, salinity, density & ocean stratification & stability Generalized depth profiles of O2 & CO2 and processes determining these profiles Forms of dissolved inorganic carbon in seawater and their buffering effect on pH of seawater Water Properties and Climate Change 2 main causes of global sea level rise, 2 main causes of local sea level rise Physical properties of water that affect sea level rise Icebergs & sea ice: Differences in sources, and effects of freezing & melting on sea level How heat content of upper ocean & Arctic sea ice extent have changed since about 1970s Invasion of fossil fuel CO2 in the oceans and effects on pH The Sea Floor & Plate Tectonics General differences in rock type & density of oceanic vs. continental crust Mantle convection process driving sea-floor spreading & plate motion Tectonic plates & relationship to deep & shallow earthquakes 3 types of plate boundaries, their relative plate motion & extent of quake & volcano activity Subduction, crust density, trenches & sediments Differences between hot spot and islands arc volcano chains Characteristics & examples of 2 types of continental margins Origins & general locations of canyons, continental rises, seamounts, abyssal plains & hills Origin & results of turbidity currents General locations & origins of hydrothermal vents & “Lost City” Geochemical processes creating hydrothermal vents & “Lost City” Atmospheric Circulation Layers of the atmosphere & their general properties Revised April 23, 2008 2 reasons for uneven distribution of solar energy striking Earth’s surface Convection, atmospheric pressure, and precipitation patterns on an idealized Earth with no rotation & no land Coriolis effect & how it changes air motions on an idealized Earth with rotation & no land Heat capacity of land vs. water and effects on continents on global & seasonal wind patterns Effects of mountains on wind & precipitation Ocean Water Column Structure & Thermohaline Circulation General geographic differences in surface temperature & density & causes General seasonal changes in depth profiles of temperature & density Temperature & salinity conditions that create convection in the oceans Regions of upwelling & downwelling, convergence & divergence in ocean convection “Global conveyor belt” and its relationship to climat change Normal vs. Niño conditions: geographic patterns of atmospheric pressure, winds, precipitation, water temperature, thermocline, currents, upwelling in the equatorial Pacific 2 monitoring systems for El Niño detection Ocean Surface Currents Processes explaining wind-driven surface current, Ekman Spiral, & net transport Sea surface elevation, currents, convergence, divergence, upwelling & downwelling driven by trade winds & westerlies Effect of continents in creating gyres Balance of pressure and Coriolis in geostrophic flow Explain processes driving major currents of N. & S. Pacific, N. & S. Atlantic gyres VOCABULARY (New words in red) Abyssal hills Abyssal plain Albedo Antarctic Bottom Water Antarctic Intermediate Water Asthenosphere Bedrock Continental rise Continental shelf Continental slope Convection Convergent boundary Divergent boundary Downwelling ENSO Geostrophic flow Gyres Halocline Heat capacity (specific heat) Indonesian Low Juan de Fuca Plate Land & sea breeze Lithosphere Magma Mid-ocean Ridge/rise Mixed layer N. Atlantic Deep Water North American Plate Ocean conveyor belt Orographic effect pH Plate tectonics Polar easterlies Polar jet stream Prevailing Westerlies Pycnocline Pycnocline Rift Valley ROV’s and AUV’s S. Pacific High Seamounts Subduction Submarine canyon Submarine canyons Subtropical jet Thermocline Thermohaline circulation Trade winds Trench Turbidity current Upwelling The exam will contain several diagrams with questions that apply to each. Questions based on a diagram like Fig. 6.5, p. 161 S&A and Fig. 8.4, p. 210 in S&A. Study: • Definitions of features on water columns profiles • Explanations of profiles & relationships among properties depicted Questions based on Fig. 8.6, p. 211 in S&A. See also Fig. 9.11, p. 238 in S&A. Study: • Processes driving thermohaline circulation, where they are most important, and why • Surface convergences & divergences and relationships to upwelling & downwelling Questions based on the geology diagram below. See also Fig. 3.29, p. 75 in S&A. Study: • Names of plates • Sea floor features (as in the in-class activity) • Types of plate boundaries and continental margins • Directions of plate motions • Volcanic & earthquake activity Questions based on the maps and narrative below. See also Figs. 7.22 & 7. 23, pp. 191 & 194 and Fig. 9.12, p. 238 in S&A. Study: • Changes in atmospheric pressure by season & causes • Relationship of atmospheric pressure & geostrophic wind direction • Ekman spiral water movement at the surface & in the Ekman layer • Upwelling & downwelling in relation to wind The cargo ship New Carissa ran aground off the Coos Bay estuary on the Oregon coast during a sudden storm on February 4, 1999 (see Figure 3). Oil began spilling from its ruptured fuel tanks and spreading across the coastal zone. Late on March 2, the broken bow section of the New Carissa‘s hull was being towed about 50 nautical miles offshore when the towline broke in a storm. The bow drifted to come aground again near the town of Waldport to the north (see map). Some of the fuel oil from the New Carissa had been in the tanks for a long time and was full of sludge. Upon entering seawater, this dense oil would sink gradually below the surface. The ship can be used as a tracer of water movement at the very surface of the water, and the oil can be used as a tracer of water movement in the Ekman layer. Ignore the effects of waves on the motion of the ship and oil. .
Load more

Recommended publications
  • Intro to Tidal Theory
    Introduction to Tidal Theory Ruth Farre (BSc. Cert. Nat. Sci.) South African Navy Hydrographic Office, Private Bag X1, Tokai, 7966 1. INTRODUCTION Tides: The periodic vertical movement of water on the Earth’s Surface (Admiralty Manual of Navigation) Tides are very often neglected or taken for granted, “they are just the sea advancing and retreating once or twice a day.” The Ancient Greeks and Romans weren’t particularly concerned with the tides at all, since in the Mediterranean they are almost imperceptible. It was this ignorance of tides that led to the loss of Caesar’s war galleys on the English shores, he failed to pull them up high enough to avoid the returning tide. In the beginning tides were explained by all sorts of legends. One ascribed the tides to the breathing cycle of a giant whale. In the late 10 th century, the Arabs had already begun to relate the timing of the tides to the cycles of the moon. However a scientific explanation for the tidal phenomenon had to wait for Sir Isaac Newton and his universal theory of gravitation which was published in 1687. He described in his “ Principia Mathematica ” how the tides arose from the gravitational attraction of the moon and the sun on the earth. He also showed why there are two tides for each lunar transit, the reason why spring and neap tides occurred, why diurnal tides are largest when the moon was furthest from the plane of the equator and why the equinoxial tides are larger in general than those at the solstices.
    [Show full text]
  • Oceanography Lecture 12
    Because, OF ALL THE ICE!!! Oceanography Lecture 12 How do you know there’s an Ice Age? i. The Ocean/Atmosphere coupling ii.Surface Ocean Circulation Global Circulation Patterns: Atmosphere-Ocean “coupling” 3) Atmosphere-Ocean “coupling” Atmosphere – Transfer of moisture to the Low latitudes: Oceans atmosphere (heat released in higher latitudes High latitudes: Atmosphere as water condenses!) Atmosphere-Ocean “coupling” In summary Latitudinal Differences in Energy Atmosphere – Transfer of moisture to the atmosphere: Hurricanes! www.weather.com Amount of solar radiation received annually at the Earth’s surface Latitudinal Differences in Salinity Latitudinal Differences in Density Structure of the Oceans Heavy Light T has a much greater impact than S on Density! Atmospheric – Wind patterns Atmospheric – Wind patterns January January Westerlies Easterlies Easterlies Westerlies High/Low Pressure systems: Heat capacity! High/Low Pressure systems: Wind generation Wind drag Zonal Wind Flow Wind is moving air Air molecules drag water molecules across sea surface (remember waves generation?): frictional drag Westerlies If winds are prolonged, the frictional drag generates a current Easterlies Only a small fraction of the wind energy is transferred to Easterlies the water surface Westerlies Any wind blowing in a regular pattern? High/Low Pressure systems: Wind generation by flow from High to Low pressure systems (+ Coriolis effect) 1) Ekman Spiral 1) Ekman Spiral Once the surface film of water molecules is set in motion, they exert a Spiraling current in which speed and direction change with frictional drag on the water molecules immediately beneath them, depth: getting these to move as well. Net transport (average of all transport) is 90° to right Motion is transferred downward into the water column (North Hemisphere) or left (Southern Hemisphere) of the ! Speed diminishes with depth (friction) generating wind.
    [Show full text]
  • Tidal and Wind-Driven Currents from Oscr
    FEATURE TIDAL AND WIND-DRIVEN CURRENTS FROM OSCR By David Prandle TWO IMPORTANTASPECTS of tidal currents are (1) be seen by comparing calculations of M, tidal vor- their temporal coherence and (2) their constancy ticity distributions <OV/OX- c?U/OY> from OSCR (over centuries). The first rigorous evaluation of an measurements with corresponding model calcula- Ocean Surface Current Radar (OSCR) system ex- tions (Prandle 1987). ploited these characteristics using sequential de- Tidal Residuals ployments of the one available unit with subse- The propagation of tidal energy from the quent combination of radial components to ocean into shelf seas produces an attendant net construct tidal ellipses (Prandle and Ryder 1985). residual current Uo of 0.5(OUD)cos 0 (0, oscil- Specifications for Tidal Mapping lating current amplitude; c, elevation amplitude: The Rayleigh criterion for separation of closely D, water depth: O, phase difference between lJ spaced constituents in tidal analysis suggests ob- and {). In U.K. waters Uo is typically 0-3 cm s ' servational periods exceeding the related beat fre- compared with 0 of 40-100 cm s ', thus conven- • . enhanced reso- quency, this dictates 15 d of observations to sepa- tional current meters often fail to resolve U~,. lution of the instru- rate the two largest constituents M~ and St. For Moreover, numerical models that accurately sim- tidal elevations this criterion is often relaxed: ulate M z may not resolve U,, with the same accu- mentation reveals however, while elevations show a noise:tidal sig- racy. Year-long deployments of OSCR, in the finer scale dynamical nal ratio of 0(0.1-0.2), the same ratio for currents Dover Straits (Prandle et al., 1993) and the North is 0(0.5).
    [Show full text]
  • Physical Oceanography - UNAM, Mexico Lecture 3: the Wind-Driven Oceanic Circulation
    Physical Oceanography - UNAM, Mexico Lecture 3: The Wind-Driven Oceanic Circulation Robin Waldman October 17th 2018 A first taste... Many large-scale circulation features are wind-forced ! Outline The Ekman currents and Sverdrup balance The western intensification of gyres The Southern Ocean circulation The Tropical circulation Outline The Ekman currents and Sverdrup balance The western intensification of gyres The Southern Ocean circulation The Tropical circulation Ekman currents Introduction : I First quantitative theory relating the winds and ocean circulation. I Can be deduced by applying a dimensional analysis to the horizontal momentum equations within the surface layer. The resulting balance is geostrophic plus Ekman : I geostrophic : Coriolis and pressure force I Ekman : Coriolis and vertical turbulent momentum fluxes modelled as diffusivities. Ekman currents Ekman’s hypotheses : I The ocean is infinitely large and wide, so that interactions with topography can be neglected ; ¶uh I It has reached a steady state, so that the Eulerian derivative ¶t = 0 ; I It is homogeneous horizontally, so that (uh:r)uh = 0, ¶uh rh:(khurh)uh = 0 and by continuity w = 0 hence w ¶z = 0 ; I Its density is constant, which has the same consequence as the Boussinesq hypotheses for the horizontal momentum equations ; I The vertical eddy diffusivity kzu is constant. ¶ 2u f k × u = k E E zu ¶z2 that is : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 Ekman currents Ekman balance : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 Ekman currents Ekman balance : ¶ 2u f k × u = k E E zu ¶z2 that is : Ekman currents Ekman balance : ¶ 2u f k × u = k E E zu ¶z2 that is : k ¶ 2v u = zu E E f ¶z2 k ¶ 2u v = − zu E E f ¶z2 ¶uh τ = r0kzu ¶z 0 with τ the surface wind stress.
    [Show full text]
  • Ocean Surface Circulation
    Ocean surface circulation Recall from Last Time The three drivers of atmospheric circulation we discussed: • Differential heating • Pressure gradients • Earth’s rotation (Coriolis) Last two show up as direct forcing of ocean surface circulation, the first indirectly (it drives the winds, also transport of heat is an important consequence). Coriolis In northern hemisphere wind or currents deflect to the right. Equator In the Southern hemisphere they deflect to the left. Major surfaceA schematic currents of them anyway Surface salinity A reasonable indicator of the gyres 31.0 30.0 32.0 31.0 31.030.0 33.0 33.0 28.0 28.029.0 29.0 34.0 35.0 33.0 33.0 33.034.035.0 36.0 34.0 35.0 37.0 35.036.0 36.0 34.0 35.0 35.0 35.0 34.0 35.0 37.0 35.0 36.0 36.0 35.0 35.0 35.0 34.0 34.0 34.0 34.0 34.0 34.0 Ocean Gyres Surface currents are shallow (a few hundred meters thick) Driving factors • Wind friction on surface of the ocean • Coriolis effect • Gravity (Pressure gradient force) • Shape of the ocean basins Surface currents Driven by Wind Gyres are beneath and driven by the wind bands . Most of wind energy in Trade wind or Westerlies Again with the rotating Earth: is a major factor in ocean and Coriolisatmospheric circulation. • It is negligible on small scales. • Varies with latitude. Ekman spiral Consider the ocean as a Wind series of thin layers. Friction Direction of Wind friction pushes on motion the top layers.
    [Show full text]
  • Large-Scale Oceanic Currents As Shallow-Water Asymptotic Solutions of the Navier-Stokes Equation in Rotating Spherical Coordinates ⁎ A
    Deep-Sea Research Part II xxx (xxxx) xxx–xxx Contents lists available at ScienceDirect Deep-Sea Research Part II journal homepage: www.elsevier.com/locate/dsr2 Large-scale oceanic currents as shallow-water asymptotic solutions of the Navier-Stokes equation in rotating spherical coordinates ⁎ A. Constantina, , R.S. Johnsonb a Faculty of Mathematics, University of Vienna, Oskar-Morgenstern-Platz 1, 1090 Vienna, Austria b School of Mathematics, Statistics and Physics, Newcastle University, Newcastle upon Tyne, NE1 7RU, United Kingdom ARTICLE INFO ABSTRACT Keywords: We show that a consistent shallow-water approximation of the incompressible Navier-Stokes equation written in Incompressible Navier-Stokes equation a spherical, rotating coordinate system produces, at leading order in a suitable limiting process, a general linear Ekman-type solution theory for wind-induced ocean currents which goes beyond the limitations of the classical Ekman spiral. In Rotating spherical coordinates particular, we obtain Ekman-type solutions which extend over large regions in both latitude and longitude; we present examples for constant and for variable eddy viscosities. We also show how an additional restriction on our solution recovers the classical Ekman solution (which is valid only locally). 1. Introduction this approach is still valid only in the neighbourhood of a point on the surface of the sphere, i.e. it is purely local. Of course, the formulation of The Ekman spiral (Ekman, 1905) is one of the foundations of physical oceanic flows in rotating, spherical coordinates is not new; see, for example, oceanography, being the basis for the discussion of ocean circulation in non- Marshall et al. (1997) and Veronis (1973).
    [Show full text]
  • Effects of the Earth's Rotation
    Effects of the Earth’s Rotation C. Chen General Physical Oceanography MAR 555 School for Marine Sciences and Technology Umass-Dartmouth 1 One of the most important physical processes controlling the temporal and spatial variations of biological variables (nutrients, phytoplankton, zooplankton, etc) is the oceanic circulation. Since the circulation exists on the earth, it must be affected by the earth’s rotation. Question: How is the oceanic circulation affected by the earth’s rotation? The Coriolis force! Question: What is the Coriolis force? How is it defined? What is the difference between centrifugal and Coriolis forces? 2 Definition: • The Coriolis force is an apparent force that occurs when the fluid moves on a rotating frame. • The centrifugal force is an apparent force when an object is on a rotation frame. Based on these definitions, we learn that • The centrifugal force can occur when an object is at rest on a rotating frame; •The Coriolis force occurs only when an object is moving relative to the rotating frame. 3 Centrifugal Force Consider a ball of mass m attached to a string spinning around a circle of radius r at a constant angular velocity ω. r ω ω Conditions: 1) The speed of the ball is constant, but its direction is continuously changing; 2) The string acts like a force to pull the ball toward the axis of rotation. 4 Let us assume that the velocity of the ball: V at t V + !V " V = !V V + !V at t + !t ! V = V!" ! V !" d V d" d" r = V , limit !t # 0, = V = V ($ ) !t !t dt dt dt r !V "! V d" V = % r, and = %, dt V Therefore, d V "! = $& 2r dt ω r To keep the ball on the circle track, there must exist an additional force, which has the same magnitude as the centripetal acceleration but in an opposite direction.
    [Show full text]
  • Lamont-Doherty Earth Observatory Insert
    ARCTIC Arctic Research Consortium of the United States Member Institution Spring/Autumn 1999 Arctic Research at Lamont-Doherty Earth Observatory Early Years of Lamont Research in the High Arctic olumbia University’s Lamont- CDoherty Earth Observatory (LDEO) entered the arena of arctic research more than four decades ago, when the Alaskan Air Command established Drifting Station A (or Alpha) on a 3 m-thick ice floe at 83° N 165° W. Station A was a U.S. con- tribution to the International Geophysical Year in 1957. Lamont scientists under the general direction of Jack Oliver and field leader- ship of Ken Hunkins conducted a pro- gram of geophysical and oceanographic research at the station, while investigators from other institutions carried out pro- grams of upper atmosphere, meteorologi- Lamont researchers have reconstructed annual temperatures for the arctic zone (65–90°N) during the past 400 years cal, sea-ice, and biological research. The using tree-ring width data from 12 sites near circumpolar treeline and three sites at northern, elevational treeline. Ten Lamont program used many instruments or more trees were sampled at each site. At all the sites, annual growth is limited by temperature. The regression used and techniques that had been developed principal component analysis to reduce the number of predictors and one forward lag of the series to account for carryover effects of temperature on tree growth. The regression explains 66% of the variance in temperature after adjustment for by Doc Ewing and other Lamont scientists degrees of freedom lost due to the regression. The tree-ring reconstruction helps quantify the unusual warming that is for exploration of the open oceans, modi- reflected in other arctic investigations.
    [Show full text]
  • The Ekman Spiral for Piecewise-Uniform Diffusivity
    https://doi.org/10.5194/os-2020-31 Preprint. Discussion started: 27 May 2020 c Author(s) 2020. CC BY 4.0 License. 1 The Ekman spiral for piecewise-uniform diffusivity 1 2 3 2 David G. Dritschel , Nathan Paldor , Adrian Constantin 1 3 School of Mathematics and Statistics, University of St Andrews, 4 St Andrews KY16 9SS, UK 2 5 The Fredy & Nadin Herrman Institue of Earth Sciences, The Hebrew University, 6 Jerusalem 9190401, Israel 3 7 Department of Mathematics, University of Vienna, 8 Vienna 1090, Austria 9 May 13, 2020 10 Abstract 11 We re-visit Ekman’s (1905) classic problem of wind-stress induced ocean currents to 12 help interpret observed deviations from Ekman’s theory, in particular from the predicted 13 surface current deflection of 45◦. While previous studies have shown that such deviations 14 can be explained by a vertical eddy viscosity varying with depth, as opposed to the 15 constant profile taken by Ekman, analytical progress has been impeded by the difficulty 16 in solving Ekman’s equation. Herein, we present a solution for piecewise-constant eddy 17 viscosity which enables a comprehensive understanding of how the surface deflection angle 18 depends on the vertical profile of eddy viscosity. For two layers, the dimensionless problem 19 depends only on the depth of the upper layer and the ratio of layer viscosities. A single 20 diagram then allows one to understand the dependence of the deflection angle on these 21 two parameters. 22 1 Introduction 23 The motion of the near-surface ocean layer is a superposition of waves, wind-driven currents 24 and geostrophic flows.
    [Show full text]
  • Deep Layer Variability in the Eastern North Atlantic the EDYLOC
    ____________________________________o_c_EA_N_O __ LO_G __ IC_A_A_C_T_A __ 19_8_8_-_v_o_L_._1_1_-_N_o_2~~~----- Current meler array Dynamics Bottom nepheloid layer Deep layer variability Variability Porcupine abyssal plain in the Eastern North Atlantic: Mouillages de courantomètres Dynamique Couche néphéloïde profonde the EDYLOC experiment Variabilité Plaine abyssale Porcupine Annick V ANGRIESHEIM Institut Français de Recherche pour l'Exploitation de la Mer (IFREMER), Centre de Brest, B. P. 70, 29263 Plouzané, France. Received 7/4/87, in revised form 19/11/87, accepted 24/11/87. ABSTRACT The ÉDYLOC ("Étude DYnamique LOCale") experiment was carried out by IFREMER-Centre de Brest in 1981-1982 in order to describe the dynamics and evaluate the space and time scales of current variability in the deep layer of the Porcupine abyssal plain (North East Atlantic). Six moorings separated by 11 to 73 km were deployed in a flat bottom area near 47°N, 14°30'W. The water depth was 4780 m. The results are described here. A hydrological survey, with nephelometry profiles, shows that a nepheloid layer exists at each station with the strongest signal associated with the only observed bottom mixed layer in the north-western part of the array; it is also there that the currents are the strongest throughout the measurement period. Over the 11 months of record (data return: 96.2%), the horizontally averaged mean speed is 1.26 cmjs at 4000 m and 1.50 cm/s at 10 m above the bottom with a predominancy of the westward-component. The correlation between the two levels is very high, which means that the deepest level dynamics is not influenced by the bottom effect to the extent that one might expect in a bottom boundary layer.
    [Show full text]
  • Oceanscoasts INDEX.Pdf
    OceansCoasts_INDEX.pdf OceansCoasts_INDEX.pdf This is an index of all terms/ideas in this question bank. Question banks are organized into topics containing related terms/ideas. Each term/idea has at least one related question, in some cases illustrated with a photo or diagram. Question names are shown in italics, followed by an abbreviated photo source. All terms are listed in the order that they occur within the actual question bank. The file name listed after "Test bank" is a lower quality, smaller image suitable for use on the web. The file name listed after "High quality" is a larger and better quality image suitable for use in classroom presentations. Additional information regarding the photo/diagram sources can be found in the OceansCoasts_Captions.pdf file. QB: Oceans and Coasts Topic 01: Ocean Characteristics – Definitions Compatible with: Marshak (Ch. 18) Terms: bathymetry – No Picture coast – No Picture continental shelf Test bank: [Oceans01_01.jpg] High quality: [Atlantic_NOAA.jpg] continental slope Test bank: [Oceans01_01.jpg] High quality: [Atlantic_NOAA.jpg] abyssal plain Test bank: [Oceans01_01.jpg] High quality: [Atlantic_NOAA.jpg] passive continental margin – example Test bank: [Oceans01_01.jpg] High quality: [Atlantic_NOAA.jpg] active continental margin – example Test bank: [Oceans01_02.jpg] High quality: [00N090W_NOAA.jpg] submarine canyons Test bank: [Oceans01_03.jpg] High quality: [Canyon_SanMonBay_CA_USGS.jpg] turbidity current – No Picture Page 1 of 10 OceansCoasts_INDEX.pdf turbidite – No Picture submarine fan Test bank: [Oceans01_03.jpg] High quality: [Canyon_SanMonBay_CA_USGS.jpg] QB: Oceans and Coasts Topic 02: Ocean Composition – Definitions Compatible with: Marshak (Ch. 18) Terms: salinity – No Picture halocline – No Picture thermocline – No Picture pycnocline – No Picture heat capacity – No Picture QB: Oceans and Coasts Topic 03: Ocean Currents – Definitions Compatible with: Marshak (Ch.
    [Show full text]
  • Coastal Upwelling TEACHER’S GUIDE
    AMERICAN METEOROLOGICAL SOCIETY The Maury Project Coastal Upwelling TEACHER’S GUIDE A The Maury Project This guide is one of a series produced by The Maury Project, an initiative of the American Meteorological Society and the United States Naval Academy. The Maury Project has created and trained a network of selected master teachers who provide peer training sessions in precollege physical oceanographic education. To support these teachers in their teacher training, The Maury Project develops and produces teacher's guides, slide sets, and other educational materials. For further information, and the names of the trained master teachers in your state or region, please contact: The Maury Project American Meteorological Society 1200 New York Avenue, NW, Suite 500 Washington, DC 20005 This material is based upon work supported by the National Science Foundation under Grant No. ESI-9353370. This project was supported, in part, by the National Science Foundation Opinions expressed are those of the authors and not necessarily those of the foundation © 2018 American Meteorological Society (Permission is hereby granted for the reproduction, without alteration, of materials contained in this publication for non-commercial use in schools on the condition their source is acknowledged.) i Forward This guide has been prepared to introduce fundamental understandings about the guide topic. This guide is organized as follows: Introduction This is a narrative summary of background information to introduce the topic. Basic Understandings Basic understandings are statements of principles, concepts, and information. The basic understandings represent material to be mastered by the learner, and can be especially helpful in devising learning activities and in writing learning objectives and test items.
    [Show full text]