1 / 16

Increasing Reynolds #

Increasing Reynolds #. Turbulence characteristics. 3-dimensional rotational – carries vorticity (unlike linear surface waves) irregular, unpredictable (random) motion – described by probability density function diffusive – several orders of magnitude greater than molecular diffusion

dysis
Télécharger la présentation

Increasing Reynolds #

An Image/Link below is provided (as is) to download presentation Download Policy: Content on the Website is provided to you AS IS for your information and personal use and may not be sold / licensed / shared on other websites without getting consent from its author. Content is provided to you AS IS for your information and personal use only. Download presentation by click this link. While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server. During download, if you can't get a presentation, the file might be deleted by the publisher.

E N D

Presentation Transcript

  1. Increasing Reynolds #

  2. Turbulence characteristics 3-dimensional rotational – carries vorticity (unlike linear surface waves) irregular, unpredictable (random) motion – described by probability density function diffusive – several orders of magnitude greater than molecular diffusion dissipative – K.E.→ heatrequires steady supply of energy

  3. Turbulence characteristics flow has large Reynolds #,(nonlinear) does not obey a dispersion relation (not wavelike) broad wavenumber spectrum generally anisotropic at larger scales is a function of the flow, not the fluid satisfies Navier-Stokes equations

  4. Dynamic Stability Concepts Figure from Thorpe Statically stable, dynamically unstable = forced convection (figure from Stull)

  5. Vertical turbulent transports What is a turbulent flux? Reynolds’ decomposition: <wT> = <w><T> + <w’T’> What determines the vertical distribution of turbulence? TKE equation: dTKE/dt = production – dissipation + advection How does turbulence determine the interfacial fluxes of heat, moisture and momentum? Near-surface gradients and TKE levels are related. How are vertical turbulent transports modeled? Flux profile relationships (Monin-Obukhov similarity theory) closure schemes (parameterizations) layered versus level models

  6. Turbulent Flux Definitions Reference Lecture 2 for bulk parameterizations of these

  7. Turbulence dissipation

  8. PBL TKE budget forced convection free convection • u* friction velocity • w* convective velocity scale • h boundary layer height • ε dissipation of TKE • S shear production of TKE • B buoyancy production/damping of TKE • T transport of TKE

  9. the flow is in steady state, i.e, • the boundary layer is horizontally homogeneous, i.e.,                      and • the boundary layer is statically neutral, i.e., • the boundary layer is barotropic, i.e., Ug and Vg are constant with height • there is no subsidence, i.e., W = 0 Ekman Flow assumptions

  10.                                                      (1) • How can we solve equation set (1)? • First, let's define the magnitude of the geostrophic wind, G by G = [U2g + V2g]0.5 • Let's also assume that the geostrophic wind is parallel to the X axis, thus: • G = Ug • V2g = 0 • Let's also use first-order local closure K-theory, assuming a constant Kmto eliminate the flux terms. • Hence:                                  (2) • Substituting (2) into (1) gives: •                                             (3) Ekman Flow

  11. Here we have a set of two partial differential equations...., how to solve????? • Well, we need to specify the boundary conditions: • U= 0 at z = 0 • V= 0 at z = 0 • U  --> G as z --> large (get above the boundary layer) • V --> 0 as z --> large (the geostrophic flow above the boundary layer is parallel to the X axis) • The solution to (3) using the above boundary conditions is: •                                                              (4)    • where Ekman Flow

  12. Ekman Flow

More Related