Frictional Damping of Baroclinic Waves
|
|
- Ronald Wilkins
- 6 years ago
- Views:
Transcription
1 Frictional Damping of Baroclinic Waves HHH, 26th May 2006 Bob Plant With thanks to Stephen Belcher, Brian Hoskins, Dan Adamson
2 Motivation Control simulation, T+60 Simulation with no boundary layer turbulence, T mb 930mb Simulations with and without boundary layer processes active for T+60 of storm on 12Z 31/10/00. Frictional Damping of Baroclinic Waves p.1/24
3 Surface Roughness Accounting for orographic and ocean wave effects has produced increased roughness in NWP The increased roughness has increased NWP skill. But how and why? (How much roughness should be there?) Has become a real issue in deciding between competing (but very different) parameterizations of orographic effects. Frictional Damping of Baroclinic Waves p.2/24
4 Some Context Potential vorticity framework Baroclinic wave studies with IGCM: LC1 and LC2 Added simple (but realistic) boundary layer scheme Three cyclones in UM (different forcing mechanisms) with careful diagnosis of PV generation by model physics Here, focus will be on LC1, with friction but no boundary layer heat fluxes Frictional Damping of Baroclinic Waves p.3/24
5 Bulk Effect of Friction R0 2 ) Eddy kinetic energy (J/m Rd Time (days) Frictional Damping of Baroclinic Waves p.4/24
6 Mechanisms for Frictional PV Generation Frictional Damping of Baroclinic Waves p.5/24
7 PV Generation (1) Average over boundary layer: DP Dt = G 1 ρ F θ, (2) D[P] Dt = [G] w hp h h + small terms. Frictional Damping of Baroclinic Waves p.6/24
8 Contributions to [G] Ekman term: (3) [G E ] = 1 ρ 2 h 2 θˆk τ s = f θ ρh 2 w E Baroclinic term: (4) [G B ] = 1 ρ 2 h 2 ˆk τ s ( H θ) h v s v T and some small terms. Frictional Damping of Baroclinic Waves p.7/24
9 Ekman Pumping Convergence over low ascent vortex-tube squashing spindown of barotropic vortex tropopause ξ 2 free troposphere ξ 1 ξ > ξ 1 2 boundary layer surface Reduces PV over the low Frictional Damping of Baroclinic Waves p.8/24
10 Baroclinic Term a) N H L H v T dθ dy Basic-state temperature gradient Perturbation surface zonal wind Frictional Damping of Baroclinic Waves p.9/24
11 Baroclinic Term For a neutral wave: b) N v T v T H L H v min v max θ min dθ dx max θ max dθ dx min Perturbation zonal temperature gradient Perturbation meridional zonal wind Frictional Damping of Baroclinic Waves p.10/24 θ min
12 Baroclinic Term Combine these and account for wave growth and frictional turning of the wind: c) N v T v T H L H v T v T v T v T Frictional Damping of Baroclinic Waves p.11/24
13 Low-level PV Evolution of the Wave Frictional Damping of Baroclinic Waves p.12/24
14 Near-Surface PV 70N 60N 50N H L P1 40N 30N 20N 105W 90W 75W 60W 45W PV at σ = 0.98 after 4 days Frictional Damping of Baroclinic Waves p.13/24
15 Where Does This Come From? 70N a) 70N b) 60N L 60N L 50N H 50N H 40N 40N 30N 30N 20N 20N 105W 90W 75W 60W 45W 105W 90W 75W Ekman (left) and baroclinic (right) generation terms 60W 45W Frictional Damping of Baroclinic Waves p.14/24
16 Comparison with the Theory 70N c) 60N L 10 m/s 50N H 40N 30N 20N 105W Near surface winds and angle between v s and v T 90W 75W 60W 45W Frictional Damping of Baroclinic Waves p.15/24
17 Transport of Generated PV 70N a) 70N b) 70N c) 60N N L 60N L P1 60N P1 L 50N P1 H 50N H 50N H 40N 40N 40N 30N 30N 30N 20N 75W 60W 45W 30W 15W 20N 75W 60W 45W 30W 15W 20N 75W 60W 45W 30W 15W PV at σ = 0.98 (left), σ = (left) and σ = 0.92 (right) after 6 days Frictional Damping of Baroclinic Waves p.16/24
18 Transport of Generated PV Negative low-level PV in vicinty of low Generated by Ekman mechanism close to low Remains localized Positive PV to north and east Generated by baroclinic mechanism Advected out of boundary layer by warm conveyor belt Frictional Damping of Baroclinic Waves p.17/24
19 How Does This Damp the Wave? Frictional Damping of Baroclinic Waves p.18/24
20 Cross Section 0.7 a) 0.8 Sigma W L 60W 45W 30W 15W PV and θ after 6 days Frictional Damping of Baroclinic Waves p.19/24
21 Stability Sigma N 20N 40N 60N 80N Zonal-mean stability after 7 days (P1 dθ ) Frictional Damping of Baroclinic Waves p.20/24
22 Estimated Stability Effects Effect on linear growth rate of Eady wave: Using resulting N 25% reduction directly from increased N 15% reduction because Rossby radius increases so that wavenumber 6 is no longer optimal Frictional Damping of Baroclinic Waves p.21/24
23 Case Study (FASTEX IOP15) PV attributed to barotropic frictional effects, T+24, 900mb Frictional Damping of Baroclinic Waves p.22/24
24 Case Study PV attributed to baroclinic frictional effects, T+24, 950 and 850mb Frictional Damping of Baroclinic Waves p.23/24
25 Conclusions Ekman pumping spins down a barotropic vortex PV is generated baroclinically on the NE of a low (robust mechanism) Positive PV carried out of boundary layer Associated static stability anomaly Case studies suggest 1/3 of PV generation from friction Frictional Damping of Baroclinic Waves p.24/24
Boundary layer controls on extratropical cyclone development
Boundary layer controls on extratropical cyclone development R. S. Plant (With thanks to: I. A. Boutle and S. E. Belcher) 28th May 2010 University of East Anglia Outline Introduction and background Baroclinic
More informationPV Generation in the Boundary Layer
1 PV Generation in the Boundary Layer Robert Plant 18th February 2003 (With thanks to S. Belcher) 2 Introduction How does the boundary layer modify the behaviour of weather systems? Often regarded as a
More informationFriction in mid latitude cyclones: an Ekman PV mechanism
Friction in mid latitude cyclones: an Ekman PV mechanism Article Accepted Version Boutle, I. A., Belcher, S. E. and Plant, R. S. (2015) Friction in mid latitude cyclones: an Ekman PV mechanism. Atmospheric
More informationNumerical Simulation of Baroclinic Waves with a Parameterized Boundary Layer
DECEMBER 2007 P L A N T A N D BELCHER 4383 Numerical Simulation of Baroclinic Waves with a Parameterized Boundary Layer R. S. PLANT AND S. E. BELCHER Joint Centre for Mesoscale Meteorology, University
More information2. Baroclinic Instability and Midlatitude Dynamics
2. Baroclinic Instability and Midlatitude Dynamics Midlatitude Jet Stream Climatology (Atlantic and Pacific) Copyright 26 Emily Shuckburgh, University of Cambridge. Not to be quoted or reproduced without
More informationNonlinear baroclinic dynamics of surface cyclones crossing a zonal jet
Nonlinear baroclinic dynamics of surface cyclones crossing a zonal jet Jean-Baptiste GILET, Matthieu Plu and Gwendal Rivière CNRM/GAME (Météo-France, CNRS) 3rd THORPEX International Science Symposium Monterey,
More information3. Midlatitude Storm Tracks and the North Atlantic Oscillation
3. Midlatitude Storm Tracks and the North Atlantic Oscillation Copyright 2006 Emily Shuckburgh, University of Cambridge. Not to be quoted or reproduced without permission. EFS 3/1 Review of key results
More informationBALANCED FLOW: EXAMPLES (PHH lecture 3) Potential Vorticity in the real atmosphere. Potential temperature θ. Rossby Ertel potential vorticity
BALANCED FLOW: EXAMPLES (PHH lecture 3) Potential Vorticity in the real atmosphere Need to introduce a new measure of the buoyancy Potential temperature θ In a compressible fluid, the relevant measure
More informationLecture 8. Lecture 1. Wind-driven gyres. Ekman transport and Ekman pumping in a typical ocean basin. VEk
Lecture 8 Lecture 1 Wind-driven gyres Ekman transport and Ekman pumping in a typical ocean basin. VEk wek > 0 VEk wek < 0 VEk 1 8.1 Vorticity and circulation The vorticity of a parcel is a measure of its
More informationIn two-dimensional barotropic flow, there is an exact relationship between mass
19. Baroclinic Instability In two-dimensional barotropic flow, there is an exact relationship between mass streamfunction ψ and the conserved quantity, vorticity (η) given by η = 2 ψ.the evolution of the
More informationChapter 2. Quasi-Geostrophic Theory: Formulation (review) ε =U f o L <<1, β = 2Ω cosθ o R. 2.1 Introduction
Chapter 2. Quasi-Geostrophic Theory: Formulation (review) 2.1 Introduction For most of the course we will be concerned with instabilities that an be analyzed by the quasi-geostrophic equations. These are
More informationChapter 9. Geostrophy, Quasi-Geostrophy and the Potential Vorticity Equation
Chapter 9 Geostrophy, Quasi-Geostrophy and the Potential Vorticity Equation 9.1 Geostrophy and scaling. We examined in the last chapter some consequences of the dynamical balances for low frequency, nearly
More informationIntroduction 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 informationEffective Depth of Ekman Layer.
5.5: Ekman Pumping Effective Depth of Ekman Layer. 2 Effective Depth of Ekman Layer. Defining γ = f/2k, we derived the solution u = u g (1 e γz cos γz) v = u g e γz sin γz corresponding to the Ekman spiral.
More information( ) (9.1.1) Chapter 9. Geostrophy, Quasi-Geostrophy and the Potential Vorticity Equation. 9.1 Geostrophy and scaling.
Chapter 9 Geostrophy, Quasi-Geostrophy and the Potential Vorticity Equation 9.1 Geostrophy and scaling. We examined in the last chapter some consequences of the dynamical balances for low frequency, nearly
More informationA Uniform PV Framework for Balanced Dynamics
A Uniform PV Framework for Balanced Dynamics vertical structure of the troposphere surface quasigeostrophic models Dave Muraki Simon Fraser University Greg Hakim University of Washington Chris Snyder NCAR
More informationDiagnosing Cyclogenesis by Partitioning Energy and Potential Enstrophy in a Linear Quasi-Geostrophic Model
Diagnosing Cyclogenesis by Partitioning Energy and Potential Enstrophy in a Linear Quasi-Geostrophic Model by Daniel Hodyss * and Richard Grotjahn Atmospheric Science Program, Dept. of Land, Air, and Water
More informationKinetic energy backscatter for NWP models and its calibration
Kinetic energy backscatter for NWP models and its calibration Glenn Shutts Met Office, Fitzroy Road EX1 3PB, United Kingdom glenn.shutts@metoffice.gov.uk ABSTRACT A form of kinetic energy backscatter (CASBS)
More informationStratospheric Processes: Influence on Storm Tracks and the NAO. Mark P. Baldwin
Stratospheric Processes: Influence on Storm Tracks and the NAO Mark P. Baldwin Mark P. Baldwin, University of Exeter Imperial College 12 December 2012 (From Baldwin and Dunkerton, Science 2001) 60 Days
More informationLecture 10a: The Hadley Cell
Lecture 10a: The Hadley Cell Geoff Vallis; notes by Jim Thomas and Geoff J. Stanley June 27 In this short lecture we take a look at the general circulation of the atmosphere, and in particular the Hadley
More informationThe Eady problem of baroclinic instability described in section 19a was shown to
0. The Charney-Stern Theorem The Eady problem of baroclinic instability described in section 19a was shown to be remarkably similar to the Rayleigh instability of barotropic flow described in Chapter 18.
More informationThe 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 informationAtmospheric dynamics and meteorology
Atmospheric dynamics and meteorology B. Legras, http://www.lmd.ens.fr/legras III Frontogenesis (pre requisite: quasi-geostrophic equation, baroclinic instability in the Eady and Phillips models ) Recommended
More information7 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 informationBoundary layer mechanisms in extratropical cyclones
QUARTERY JOURNA OF THE ROYA METEOROOGICA SOCIETY Q. J. R. Meteorol. Soc. 33: 53 55 (7) Published online in Wiley InterScience (www.interscience.wiley.com) DOI:./qj.3 Boundary layer mechanisms in extratropical
More informationFinal Examination, MEA 443 Fall 2008, Lackmann
Place an X here to count it double! Name: Final Examination, MEA 443 Fall 2008, Lackmann If you wish to have the final exam count double and replace your midterm score, place an X in the box above. As
More informationtransport & mixing of chemical airmasses in idealized baroclinic lifecycles Gavin ESLER & LMP
transport & mixing of chemical airmasses in idealized baroclinic lifecycles Gavin ESLER & LMP background synoptic scale eddies important for transport (tracers and water vapor) in the atmosphere a lot
More informationHow does stratospheric polar vortex variability affect surface weather? Mark Baldwin and Tom Clemo
How does stratospheric polar vortex variability affect surface weather? Mark Baldwin and Tom Clemo Mark P. Baldwin, University of Exeter Imperial College 12 December 2012 a Observed Average Surface Pressure
More informationDiabatic processes and the structure of the warm conveyor belt
2 nd European Windstorm Workshop Leeds, 3-4 September 2012 Diabatic processes and the structure of the warm conveyor belt Oscar Martínez-Alvarado J. Chagnon, S. Gray, R. Plant, J. Methven Department of
More informationRotating stratified turbulence in the Earth s atmosphere
Rotating stratified turbulence in the Earth s atmosphere Peter Haynes, Centre for Atmospheric Science, DAMTP, University of Cambridge. Outline 1. Introduction 2. Momentum transport in the atmosphere 3.
More informationQuasi-geostrophic ocean models
Quasi-geostrophic ocean models March 19, 2002 1 Introduction The starting point for theoretical and numerical study of the three dimensional large-scale circulation of the atmosphere and ocean is a vorticity
More informationThe 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 informationNote that Rossby waves are tranverse waves, that is the particles move perpendicular to the direction of propagation. f up, down (clockwise)
Ocean 423 Rossby waves 1 Rossby waves: Restoring force is the north-south gradient of background potential vorticity (f/h). That gradient can be due to either the variation in f with latitude, or to a
More informationQuasi-equilibrium Theory of Small Perturbations to Radiative- Convective Equilibrium States
Quasi-equilibrium Theory of Small Perturbations to Radiative- Convective Equilibrium States See CalTech 2005 paper on course web site Free troposphere assumed to have moist adiabatic lapse rate (s* does
More informationEddy PV Fluxes in a One Dimensional Model of Quasi-Geostrophic Turbulence
Eddy PV Fluxes in a One Dimensional Model of Quasi-Geostrophic Turbulence Christos M.Mitas Introduction. Motivation Understanding eddy transport of heat and momentum is crucial to developing closure schemes
More informationOn the effect of forward shear and reversed shear baroclinic flows for polar low developments. Thor Erik Nordeng Norwegian Meteorological Institute
On the effect of forward shear and reversed shear baroclinic flows for polar low developments Thor Erik Nordeng Norwegian Meteorological Institute Outline Baroclinic growth a) Normal mode solution b) Initial
More informationDynamics 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 informationDynamics of the Zonal-Mean, Time-Mean Tropical Circulation
Dynamics of the Zonal-Mean, Time-Mean Tropical Circulation First consider a hypothetical planet like Earth, but with no continents and no seasons and for which the only friction acting on the atmosphere
More informationGeophysics 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 informationMeasurement of Rotation. Circulation. Example. Lecture 4: Circulation and Vorticity 1/31/2017
Lecture 4: Circulation and Vorticity Measurement of Rotation Circulation Bjerknes Circulation Theorem Vorticity Potential Vorticity Conservation of Potential Vorticity Circulation and vorticity are the
More informationScales of Linear Baroclinic Instability and Macroturbulence in Dry Atmospheres
JUNE 2009 M E R L I S A N D S C H N E I D E R 1821 Scales of Linear Baroclinic Instability and Macroturbulence in Dry Atmospheres TIMOTHY M. MERLIS AND TAPIO SCHNEIDER California Institute of Technology,
More informationResponse of Baroclinic Life Cycles to Barotropic Shear
VOL. 55, NO. 3 JOURNAL OF THE ATMOSPHERIC SCIENCES 1FEBRUARY 1998 Response of Baroclinic Life Cycles to Barotropic Shear DENNIS L. HARTMANN AND PETER ZUERCHER Department of Atmospheric Sciences, University
More informationt tendency advection convergence twisting baroclinicity
RELATIVE VORTICITY EQUATION Newton s law in a rotating frame in z-coordinate (frictionless): U + U U = 2Ω U Φ α p U + U U 2 + ( U) U = 2Ω U Φ α p Applying to both sides, and noting ω U and using identities
More informationMicrophysical heating rates and PV modification in a warm conveyor belt: Comparison of a COSMO and IFS simulation
Microphysical heating rates and PV modification in a warm conveyor belt: Comparison of a COSMO and IFS simulation Montreal, August 18th 2014 H. Joos1, M. Böttcher1, R. Forbes2 and H. Wernli1 1) IAC, ETH
More informationThe Impact of the Extratropical Transition of Typhoon Dale (1996) on the Early Wintertime Stratospheric Circulation
The Impact of the Extratropical Transition of Typhoon Dale (1996) on the Early 1996-97 Wintertime Stratospheric Circulation Andrea L. Lang 1, Jason M. Cordeira 2, Lance F. Bosart 1 and Daniel Keyser 1
More informationDiabatic processes and the structure of extratropical cyclones
Geophysical and Nonlinear Fluid Dynamics Seminar AOPP, Oxford, 23 October 2012 Diabatic processes and the structure of extratropical cyclones Oscar Martínez-Alvarado R. Plant, J. Chagnon, S. Gray, J. Methven
More informationSynoptic-Dynamic Meteorology in Midlatitudes
Synoptic-Dynamic Meteorology in Midlatitudes VOLUME II Observations and Theory of Weather Systems HOWARD B. BLUESTEIN New York Oxford OXFORD UNIVERSITY PRESS 1993 Contents 1. THE BEHAVIOR OF SYNOPTIC-SCALE,
More informationChapter 1. Introduction
Chapter 1. Introduction In this class, we will examine atmospheric phenomena that occurs at the mesoscale, including some boundary layer processes, convective storms, and hurricanes. We will emphasize
More informationSchematic from Vallis: Rossby waves and the jet
Schematic from Vallis: Rossby waves and the jet Schematic from Vallis: Rossby waves and the jet A Barotropic Model Stochastic stirring + linear damping Force barotropic vort. eqn. with white noise in storm
More informationHow does the stratosphere influence the troposphere in mechanistic GCMs?
How does the stratosphere influence the troposphere in mechanistic GCMs? Walt Robinson Department of Atmospheric Sciences University of Illinois at Urbana-Champaign Acknowledgments: Dr. Yucheng Song, Climate
More informationBaroclinic Adjustment in an Atmosphere Ocean Thermally Coupled Model: The Role of the Boundary Layer Processes
2710 J O U R N A L O F T H E A T M O S P H E R I C S C I E N C E S VOLUME 68 Baroclinic Adjustment in an Atmosphere Ocean Thermally Coupled Model: The Role of the Boundary Layer Processes YANG ZHANG School
More informationMesoscale analysis of a comma cloud observed during FASTEX
Meteorol. Appl. 7, 129 134 (2000) Mesoscale analysis of a comma cloud observed during FASTEX K D Williams, Joint Centre for Mesoscale Meteorology, Department of Meteorology, University of Reading, PO Box
More informationReynolds Averaging. We separate the dynamical fields into slowly varying mean fields and rapidly varying turbulent components.
Reynolds Averaging Reynolds Averaging We separate the dynamical fields into sloly varying mean fields and rapidly varying turbulent components. Reynolds Averaging We separate the dynamical fields into
More informationThe Effects of Variations in Jet Width on the Growth of Baroclinic Waves: Implications for Midwinter Pacific Storm Track Variability
1JANUARY 2004 HARNIK AND CHANG 23 The Effects of Variations in Jet Width on the Growth of Baroclinic Waves: Implications for Midwinter Pacific Storm Track Variability NILI HARNIK Lamont-Doherty Earth Observatory,
More informationThe General Circulation of the Atmosphere: A Numerical Experiment
The General Circulation of the Atmosphere: A Numerical Experiment Norman A. Phillips (1956) Presentation by Lukas Strebel and Fabian Thüring Goal of the Model Numerically predict the mean state of the
More informationDiagnosis of a Quasi-Geostrophic 2-Layer Model Aaron Adams, David Zermeño, Eunsil Jung, Hosmay Lopez, Ronald Gordon, Ting-Chi Wu
Diagnosis of a Quasi-Geostrophic 2-Layer Model Aaron Adams, David Zermeño, Eunsil Jung, Hosmay Lopez, Ronald Gordon, Ting-Chi Wu Introduction For this project we use a simple two layer model, which is
More informationIsentropic Analysis. Much of this presentation is due to Jim Moore, SLU
Isentropic Analysis Much of this presentation is due to Jim Moore, SLU Utility of Isentropic Analysis Diagnose and visualize vertical motion - through advection of pressure and system-relative flow Depict
More informationTraveling planetary-scale Rossby waves in the winter stratosphere: The role of tropospheric baroclinic instability
GEOPHYSICAL RESEARCH LETTERS, VOL.???, XXXX, DOI:.29/, 1 2 Traveling planetary-scale Rossby waves in the winter stratosphere: The role of tropospheric baroclinic instability Daniela I.V. Domeisen, 1 R.
More information8 Mechanisms for tropical rainfall responses to equatorial
8 Mechanisms for tropical rainfall responses to equatorial heating More reading: 1. Hamouda, M. and Kucharski, F. (2019) Ekman pumping Mechanism driving Precipitation anomalies in Response to Equatorial
More informationA Truncated Model for Finite Amplitude Baroclinic Waves in a Channel
A Truncated Model for Finite Amplitude Baroclinic Waves in a Channel Zhiming Kuang 1 Introduction To date, studies of finite amplitude baroclinic waves have been mostly numerical. The numerical models,
More informationu g z = g T y (1) f T Margules Equation for Frontal Slope
Margules Equation for Frontal Slope u g z = g f T T y (1) Equation (1) is the thermal wind relation for the west wind geostrophic component of the flow. For the purposes of this derivation, we assume that
More informationATMOSPHERIC AND OCEANIC FLUID DYNAMICS
ATMOSPHERIC AND OCEANIC FLUID DYNAMICS Fundamentals and Large-scale Circulation G E O F F R E Y K. V A L L I S Princeton University, New Jersey CAMBRIDGE UNIVERSITY PRESS An asterisk indicates more advanced
More informationGoverning Equations and Scaling in the Tropics
Governing Equations and Scaling in the Tropics M 1 ( ) e R ε er Tropical v Midlatitude Meteorology Why is the general circulation and synoptic weather systems in the tropics different to the those in the
More informationROSSBY WAVE PROPAGATION
ROSSBY WAVE PROPAGATION (PHH lecture 4) The presence of a gradient of PV (or q.-g. p.v.) allows slow wave motions generally called Rossby waves These waves arise through the Rossby restoration mechanism,
More informationSensitivity of zonal-mean circulation to air-sea roughness in climate models
Sensitivity of zonal-mean circulation to air-sea roughness in climate models Inna Polichtchouk & Ted Shepherd Royal Meteorological Society National Meeting 16.11.2016 MOTIVATION Question: How sensitive
More informationThe Effect of Lower Stratospheric Shear on Baroclinic Instability
FEBRUARY 2007 W I T T M A N E T A L. 479 The Effect of Lower Stratospheric Shear on Baroclinic Instability MATTHEW A. H. WITTMAN AND ANDREW J. CHARLTON Department of Applied Physics and Applied Mathematics,
More informationIsland Wakes in Shallow Water
Island Wakes in Shallow Water Changming Dong, James C. McWilliams, et al Institute of Geophysics and Planetary Physics, University of California, Los Angeles 1 ABSTRACT As a follow-up work of Dong et al
More informationp. 4, 1 st two lines should read: k-hat unit vector maintains right angles with the horizontal unit vectors.
Reprinted with corrections August 2012. p. x, 2 nd column, 1 st full paragraph should read: In working to improve the text, constructive and insightful suggestions were provided by many colleagues, including
More informationIsentropic 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 informationInfluence of forced near-inertial motion on the kinetic energy of a nearly-geostrophic flow
Abstract Influence of forced near-inertial motion on the kinetic energy of a nearly-geostrophic flow Stephanne Taylor and David Straub McGill University stephanne.taylor@mail.mcgill.ca The effect of forced
More informationThe Tropospheric Jet Response to Prescribed Zonal Forcing in an Idealized Atmospheric Model
2254 J O U R N A L O F T H E A T M O S P H E R I C S C I E N C E S VOLUME 65 The Tropospheric Jet Response to Prescribed Zonal Forcing in an Idealized Atmospheric Model GANG CHEN Program in Atmospheres,
More informationEquatorial Superrotation on Tidally Locked Exoplanets
Equatorial Superrotation on Tidally Locked Exoplanets Adam P. Showman University of Arizona Lorenzo M. Polvani Columbia University Synopsis Most 3D atmospheric circulation models of tidally locked exoplanets
More informationChapter 9. Barotropic Instability. 9.1 Linearized governing equations
Chapter 9 Barotropic Instability The ossby wave is the building block of low ossby number geophysical fluid dynamics. In this chapter we learn how ossby waves can interact with each other to produce a
More information8 Baroclinic Instability
8 Baroclinic Instability The previous sections have examined in detail the dynamics behind quas-geostrophic motions in the atmosphere. That is motions that are of large enough scale and long enough timescale
More informationFixed Rossby Waves: Quasigeostrophic Explanations and Conservation of Potential Vorticity
Fixed Rossby Waves: Quasigeostrophic Explanations and Conservation of Potential Vorticity 1. Observed Planetary Wave Patterns After upper air observations became routine, it became easy to produce contour
More informationThe Key Role of Lower-Level Meridional Shear in Baroclinic Wave Life Cycles
389 The Key Role of Lower-Level Meridional Shear in Baroclinic Wave Life Cycles DENNIS L. HARTMANN Department of Atmospheric Sciences, University of Washington, Seattle, Washington (Manuscript received
More informationA Proposed Test Suite for Atmospheric Model Dynamical Cores
A Proposed Test Suite for Atmospheric Model Dynamical Cores Christiane Jablonowski (cjablono@umich.edu) University of Michigan, Ann Arbor PDEs on the Sphere Workshop Monterey, CA, June/26-29/2006 Motivation
More informationHurricanes are intense vortical (rotational) storms that develop over the tropical oceans in regions of very warm surface water.
Hurricanes: Observations and Dynamics Houze Section 10.1. Holton Section 9.7. Emanuel, K. A., 1988: Toward a general theory of hurricanes. American Scientist, 76, 371-379 (web link). http://ww2010.atmos.uiuc.edu/(gh)/guides/mtr/hurr/home.rxml
More informationGEF 1100 Klimasystemet. Chapter 7: Balanced flow
GEF1100 Autumn 2016 27.09.2016 GEF 1100 Klimasystemet Chapter 7: Balanced flow Prof. Dr. Kirstin Krüger (MetOs, UiO) 1 Lecture Outline Ch. 7 Ch. 7 Balanced flow 1. Motivation 2. Geostrophic motion 2.1
More informationModel equations for planetary and synoptic scale atmospheric motions associated with different background stratification
Model equations for planetary and synoptic scale atmospheric motions associated with different background stratification Stamen Dolaptchiev & Rupert Klein Potsdam Institute for Climate Impact Research
More information1/27/2010. With this method, all filed variables are separated into. from the basic state: Assumptions 1: : the basic state variables must
Lecture 5: Waves in Atmosphere Perturbation Method With this method, all filed variables are separated into two parts: (a) a basic state part and (b) a deviation from the basic state: Perturbation Method
More informationExamples of Pressure Gradient. Pressure Gradient Force. Chapter 7: Forces and Force Balances. Forces that Affect Atmospheric Motion 2/2/2015
Chapter 7: Forces and Force Balances Forces that Affect Atmospheric Motion Fundamental force - Apparent force - Pressure gradient force Gravitational force Frictional force Centrifugal force Forces that
More informationThe stratospheric response to extratropical torques and its relationship with the annular mode
The stratospheric response to extratropical torques and its relationship with the annular mode Peter Watson 1, Lesley Gray 1,2 1. Atmospheric, Oceanic and Planetary Physics, Oxford University 2. National
More informationDependence of Singular Vector Structure and Evolution on the Choice of Norm
1NOVEMBER 00 KIM AND MORGAN 3099 Dependence of Singular Vector Structure and Evolution on the Choice of Norm HYUN MEE KIM AND MICHAEL C. MORGAN Department of Atmospheric and Oceanic Sciences, University
More informationTransient/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 informationAnalysis of an Idealized, Three-Dimensional Diabatic Rossby Vortex: A Coherent Structure of the Moist Baroclinic Atmosphere
AUGUST 2005 M O O R E A N D M O N T G O M E R Y 2703 Analysis of an Idealized, Three-Dimensional Diabatic Rossby Vortex: A Coherent Structure of the Moist Baroclinic Atmosphere RICHARD W. MOORE AND MICHAEL
More informationInstability of a coastal jet in a two-layer model ; application to the Ushant front
Instability of a coastal jet in a two-layer model ; application to the Ushant front Marc Pavec (1,2), Xavier Carton (1), Steven Herbette (1), Guillaume Roullet (1), Vincent Mariette (2) (1) UBO/LPO, 6
More informationChapter 3. Stability theory for zonal flows :formulation
Chapter 3. Stability theory for zonal flows :formulation 3.1 Introduction Although flows in the atmosphere and ocean are never strictly zonal major currents are nearly so and the simplifications springing
More informationBoundary Layers: Homogeneous Ocean Circulation
Boundary Layers: Homogeneous Ocean irculation Lecture 7 by Angel Ruiz-Angulo The first explanation for the western intensification of the wind-driven ocean circulation was provided by Henry Stommel (948).
More informationSIO 210: Dynamics VI (Potential vorticity) L. Talley Fall, 2014 (Section 2: including some derivations) (this lecture was not given in 2015)
SIO 210: Dynamics VI (Potential vorticity) L. Talley Fall, 2014 (Section 2: including some derivations) (this lecture was not given in 2015) Variation of Coriolis with latitude: β Vorticity Potential vorticity
More informationHigh-resolution Global Climate Modeling of Saturn s and Jupiter s tropospheric and stratospheric circulations
High-resolution Global Climate Modeling of Saturn s and Jupiter s tropospheric and stratospheric circulations Aymeric SPIGA, S. Guerlet, E. Millour, Y. Meurdesoif (LSCE/CEA), M. Indurain, S. Cabanes, M.
More informationTropical cyclones in ver/cal shear: dynamic, kinema/c, and thermodynamic aspects of intensity modification
Tropical cyclones in ver/cal shear: dynamic, kinema/c, and thermodynamic aspects of intensity modification Michael Riemer 1, Michael T. Montgomery 2,3, Mel E. Nicholls 4 1 Johannes Gutenberg-Universität,
More informationPart-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 informationCHAPTER 8 NUMERICAL SIMULATIONS OF THE ITCZ OVER THE INDIAN OCEAN AND INDONESIA DURING A NORMAL YEAR AND DURING AN ENSO YEAR
CHAPTER 8 NUMERICAL SIMULATIONS OF THE ITCZ OVER THE INDIAN OCEAN AND INDONESIA DURING A NORMAL YEAR AND DURING AN ENSO YEAR In this chapter, comparisons between the model-produced and analyzed streamlines,
More informationPart 4. Atmospheric Dynamics
Part 4. Atmospheric Dynamics We apply Newton s Second Law: ma =Σ F i to the atmosphere. In Cartesian coordinates dx u = dt dy v = dt dz w = dt 1 ai = F m i i du dv dw a = ; ay = ; az = x dt dt dt 78 Coordinate
More informationBy convention, C > 0 for counterclockwise flow, hence the contour must be counterclockwise.
Chapter 4 4.1 The Circulation Theorem Circulation is a measure of rotation. It is calculated for a closed contour by taking the line integral of the velocity component tangent to the contour evaluated
More informationDynamics of the Atmosphere. Large-scale flow with rotation and stratification
12.810 Dynamics of the Atmosphere Large-scale flow with rotation and stratification Visualization of meandering jet stream Upper level winds from June 10th to July 8th 1988 from MERRA Red shows faster
More informationESCI 343 Atmospheric Dynamics II Lesson 11 - Rossby Waves
ESCI 343 Atmospheric Dynamics II Lesson 11 - Rossby Waves Reference: An Introduction to Dynamic Meteorology (4 rd edition), J.R. Holton Atmosphere-Ocean Dynamics, A.E. Gill Fundamentals of Atmospheric
More informationEffect of Topography on the Propagation of Extratropical Cyclones over the Rocky Mountains
University of Alabama in Huntsville ATS740 Final Project Effect of Topography on the Propagation of Extratropical Cyclones over the Rocky Mountains Author: Brian Freitag December 9, 2013 1. Introduction
More informationSpherical Shallow Water Turbulence: Cyclone-Anticyclone Asymmetry, Potential Vorticity Homogenisation and Jet Formation
Spherical Shallow Water Turbulence: Cyclone-Anticyclone Asymmetry, Potential Vorticity Homogenisation and Jet Formation Jemma Shipton Department of Atmospheric, Oceanic and Planetary Physics, University
More information