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Geophysical fluid dynamics

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Title: Geophysical fluid dynamics  
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Subject: Mathematical geophysics, Outline of geophysics, Geophysics, Physical oceanography, Taylor–Goldstein equation
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Geophysical fluid dynamics

Model forecast of Hurricane Mitch created by the Geophysical Fluid Dynamics Laboratory. The arrows are wind vectors and the grey shading indicates an equivalent potential temperature surface that highlights the surface inflow layer and eyewall region.

Geophysical fluid dynamics is the study of naturally occurring, large-scale flows on Earth and other planets. It is applied to the motion of fluids in the ocean and outer core, and to gases in the atmosphere of Earth and other planets. Two features that are common to many of the phenomena studied in geophysical fluid dynamics are rotation of the fluid due to the planetary rotation and stratification (layering). The applications of geophysical fluid dynamics do not generally include the circulation of the mantle, which is the subject of geodynamics, or fluid phenomena in the magnetosphere. Smaller scale flow features (those negligibly influenced by the rotation of the Earth) are the province of fields such as hydrology, physical oceanography and meteorology.[1]

Contents

  • Fundamentals 1
  • Buoyancy and stratification 2
    • Barotropic waves 2.1
  • Rotation 3
  • General circulation 4
  • See also 5
  • References 6
  • Further reading 7
  • External links 8

Fundamentals

To describe the flow of geophysical fluids, equations are needed for conservation of momentum (or Newton's second law) and conservation of energy. The former leads to the Navier-Stokes equations. Further approximations are generally made. First, the fluid is assumed to be incompressible. Remarkably, this works well even for a highly compressible fluid like air as long as sound and shock waves can be ignored. Second, the fluid is assumed to be a Newtonian fluid, meaning that there is a linear relation between the shear stress τ and the strain u, for example

\tau = \mu \frac{d u}{d x},

where μ is the viscosity. Under these assumptions the Navier-Stokes equations are

\overbrace{\rho \Big( \underbrace{\frac{\partial \mathbf{v}}{\partial t}}_{ \begin{smallmatrix} \text{Eulerian}\\ \text{acceleration} \end{smallmatrix}} + \underbrace{\mathbf{v} \cdot \nabla \mathbf{v}}_{ \begin{smallmatrix} \text{Advection} \end{smallmatrix}}\Big)}^{\text{Inertia (per volume)}} = \overbrace{\underbrace{-\nabla p}_{ \begin{smallmatrix} \text{Pressure} \\ \text{gradient} \end{smallmatrix}} + \underbrace{\mu \nabla^2 \mathbf{v}}_{\text{Viscosity}}}^{\text{Divergence of stress}} + \underbrace{\mathbf{f}}_{ \begin{smallmatrix} \text{Other} \\ \text{body} \\ \text{forces} \end{smallmatrix}}.

The left hand side represents the acceleration that a small parcel of fluid would experience in a reference frame that moved with the parcel (a Lagrangian frame of reference). In a stationary (Eulerian) frame of reference, this acceleration is divided into the local rate of change of velocity and advection, a measure of the rate of flow in or out of a small region.[2]

The equation for energy conservation is essentially an equation for heat flow. If heat is transported by conduction, the heat flow is governed by a diffusion equation. If there are also buoyancy effects, for example hot air rising, then natural convection can occur.

Buoyancy and stratification

Fluid that is less dense than its surroundings tends to rise until it has the same density as its surroundings. If there is not much energy input to the system, it will tend to become stratified. On a large scale, Earth's atmosphere is divided into a series of layers. Going upwards from the ground, these are the troposphere, stratosphere, mesosphere, thermosphere, and exosphere.

The density of air is mainly determined by temperature and water vapor content, the density of sea water by temperature and salinity, and the density of lake water by temperature. Where stratification occurs, there may be thin layers in which temperature or some other property changes more rapidly with height or depth than the surrounding fluid. Depending on the main sources of buoyancy, this layer may be called a pycnocline (density), thermocline (temperature), halocline (salinity), or chemocline (chemistry, including oxygenation).

The same buoyancy that gives rise to stratification also drives gravity waves. If the gravity waves occur within the fluid, they are called internal waves.

In modeling buoyancy-driven flows, the Navier-Stokes equations are modified using the Boussinesq approximation. This ignores variations in density except where they are multiplied by the gravitational acceleration g.

If the pressure depends only on density and vice versa, the fluid dynamics are called barotropic. In the atmosphere, this corresponds to a lack of fronts, as in the tropics. If there are fronts, the flow is baroclinic, and instabilities such as cyclones can occur.[3]

Barotropic waves

Rotation

General circulation

See also

References

  1. ^ Pedlosky 1987, pages 1-2
  2. ^ Tritton 1990
  3. ^ Haby, Jeff. "Barotropic and baroclinic defined". Haby's weather forecasting hints. Retrieved September 2011. 

Further reading

  • Cushman-Roisin, Benoit; Beckers, Jean-Marie (October 2011). Introduction to Geophysical Fluid Dynamics: Physical and Numerical Aspects (Second ed.).  
  • Gill, Adrian E. (1982). Atmosphere : Ocean dynamics. ([Nachdr.]. ed.). New York: Academic Press.  
  • McWilliams, James C. (2011). Fundamentals of geophysical fluid dynamics (1st pbk. ed.). Cambridge: Cambridge University Press.  
  • Monin, A.S. (1990). Theoretical Geophysical Fluid Dynamics. Dordrecht: Springer Netherlands.  
  • Pedlosky, Joseph (1987). Geophysical Fluid Dynamics (Second ed.).  
  • Salmon, R. (1998). Lectures on Geophysical Fluid Dynamics. Oxford University Press.
  • Tritton, D. J. (1990). Physical Fluid Dynamics (Second ed.).  
  • Vallis, Geoffrey K. (2006). Atmospheric and oceanic fluid dynamics : fundamentals and large-scale circulation (Reprint. ed.). Cambridge: Cambridge University Press.  

External links

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