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Chapter 7 Some Mathematics: The Equations of Motion Physical oceanography Instructor: Dr. Cheng-Chien Liu Department of Earth Sciences National Cheng Kung University Last updated: 24 October 2003 Introduction  Response of a fluid to • Internal force • External force   basic equations of ocean dynamics • Chapter 8: viscosity • Chapter 12: vorticity  Table 7.1 • Conservation laws  basic equations Dominant Forces for Ocean Dynamics  Gravity Fg • Wwater  P(x)  P • Revolution and rotation  DFg  tides, tidal current, tidal mixing  Buoyancy FB • DT  Dr  FB (vertical direction)  upward or sink  Wind Fw • Wind blows  momentum transfer  turbulence  ML • Wind blows  P(x)  P  waves Dominant Forces for Ocean Dynamics (cont.)  Pseudo-forces •  motion in curvilinear or rotating coordinate systems • a body moving at constant velocity seems to change direction when viewed from a rotating coordinate system  the Coriolis force  Coriolis Force • The dominant pseudo-force influencing currents  Other forces: Table 7.2 • Atmospheric pressure • Seismic Coordinate System  Coordinate System  find location  Cartesian Coordinate System • Most commonly use • Simpler  spherical coordinates • Convention: x is to the east, y is to the north, and z is up.  f-plane • Fcor = const (a Cartesian coordinate system) Describing flow in small regions Coordinate System (cont.)  b-plane • Fcor  latitude (a Cartesian coordinate system) Describing flow over areas as large as ocean basins  Spherical coordinates • (r, q, f) Describe flows that extend over large distances and in numerical calculations of basin and global scale flows Types of Flow in the Ocean  Flow due to currents • General Circulation The permanent, time-averaged circulation • Meridional Overturning Circulation The sinking and spreading of cold water Also known as the Thermohaline Circulation  the vertical movements of ocean water masses  Dr  DT and DS The circulation in meridional plane driven by mixing • Wind-Driven Circulation The circulation in the upper kilometer  wind • Gyres Wind-driven cyclonic or anti-cyclonic currents with dimensions nearly that of ocean basins. Types of Flow in the Ocean (cont.)  Flow due to currents (cont.) • Boundary Currents Currents owing parallel to coasts  Western boundary currents  fast, narrow jets  e.g. the Gulf Stream and Kuroshio  Eastern boundary currents  weak  e.g. the California Current • Squirts or Jets Long narrow currents  with dimensions of a few hundred kilometers  Nearly  west coasts • Mesoscale Eddies Turbulent or spinning flows on scales of a few hundred kilometers Types of Flow in the Ocean (cont.)  Oscillatory flows due to waves • Planetary Waves The rotation of the Earth  restoring force Including Rossby, Kelvin, Equatorial, and Yanai waves • Surface Waves (gravity waves) The waves that eventually break on the beach The large Dr between air and water  restoring force • Internal Waves Subsea wave ~ surface waves r = r (D)  restoring force • Tsunamis Surface waves with periods near 15 minutes generated by earthquakes Types of Flow in the Ocean (cont.)  Oscillatory flows due to waves (cont.) • Tidal Currents  tidal potential • Shelf Waves Periods  a few minutes Confined to shallow regions near shore The amplitude of the waves drops off exponentially with distance from shore Conservation of Mass and Salt  Dm = 0 & DS = 0  net fresh water loss  minimum flushing time • Net fresh water loss = R + P – E QL  bulk formula  large amount of ship measurements (T, q, …)  impossible • • • • Dm = 0  Vi + R + P = Vo + E DS = 0  ri Vi Si = ro Vo So Measure Vi assume ri  ro Estimate the minimum flushing time  Example • Fig 7.2: Box model  qout = q/t dt + q/x dx + qin The Total Derivative (D/Dt)  D/Dt = /dt + u( ) • A simple example of acceleration of flow in a small box of fluid • qout = q/t dt + q/x dx + qin • Dq/Dt = q/t + u q/x • 3D case: D/Dt = /t + u/x + v/y + w/z • The simple transformation of coordinates from one following a particle to one fixed in space converts a simple linear derivative into a nonlinear partial derivative Conservation of Momentum: Navier-Stokes equation  Newton’s 2nd law • F = D(mv)/Dt • Dv/Dt = F/m = fm = fp+ fc+ fg + fr Pressure gradient fp = -p/r Coriolis force fc = -2W  v  W = 7.292  10-5 radians/s Gravity fg = g Friction fr • Dv/Dt = -p/r -2W  v + g + fr W = 7.292  10-5 radians/s Conservation of Momentum: Navier-Stokes equation (cont.)  Pressure term • ax = -(1/r) (p/x) dFx = p dy dz-(p + dp) dy dz = -dp dy dz Source:http://oceanworld.tamu.edu/resources/ocng_textbook/chapter07/chapter07_06.htm Conservation of Momentum: Navier-Stokes equation (cont.)  Gravity term • g = gf - W  (W  R) Source:http://oceanworld.tamu.edu/resources/ocng_textbook/chapter07/chapter07_06.htm Conservation of Momentum: Navier-Stokes equation (cont.)  The Coriolis term Conservation of Momentum: Navier-Stokes equation (cont.)  Momentum Equation in Cartesian Coordinates Conservation of mass: the continuity equation  For compressible fluid Source:http://oceanworld.tamu.edu/resources/ocng_textbook/chapter07/chapter07_06.htm Conservation of mass: the continuity equation (cont.)  Oceanic flows are incompressible • Boussinesq's assumption v << c (sound speed)  When v  c, Dv  Dr Phase speed of waves << c  c   in incompressible flows Vertical scale of the motion << c2/g  The increase in pressure produces only small changes in density • r  const, except the pressure term (rg) Conservation of mass: the continuity equation (cont.)  For incompressible flow • The coefficient of compressibility b  b = 0 for incompressible flows Solutions to the Equations of Motion  Solvable in principle • Four equations 3 momentum equations 1 continuity equation • Four unknowns 3 velocity components: u, v, w 1 pressure p • Boundary conditions No slip condition: v//(boundary) = 0 No penetration condition: v(boundary) = 0 Solutions to the Equations of Motion (cont.)  Difficult to solve in practice • Exact solution No exact solutions for the equations with friction Very few exact solutions for the equations without friction • Analytic solution For much simplified forms of the equations of motion • Numerical solution Solutions for oceanic flows with realistic coasts and bathymetric features must be obtained from numerical solutions (Chapter 15) Important concepts • Gravity, buoyancy, and wind are the dominant forces acting on the ocean • Earth's rotation produces a pseudo force, the Coriolis force • Conservation laws applied to flow in the ocean lead to equations of motion; conservation of salt, volume and other quantities can lead to deep insights into oceanic flow Important concepts (cont.) • The transformation from equations of motion applied to fluid parcels to equations applied at a fixed point in space greatly complicates the equations of motion. The linear, first-order, ordinary differential equations describing Newtonian dynamics of a mass accelerated by a force become nonlinear, partial differential equations of fluid mechanics. • Flow in the ocean can be assumed to be incompressible except when de-scribing sound. Density can be assumed to be constant except when density is multiplied by gravity g. The assumption is called the Boussinesq approximation Important concepts (cont.) • Conservation of mass leads to the continuity equation, which has an especially simple form for an incompressible fluid.
 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
									 
                                             
                                             
                                             
                                             
                                             
                                             
                                             
                                             
                                             
                                             
                                            