- 100 Views
- Uploaded on
- Presentation posted in: General

Marine Turbulence and Mixing

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.While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server.

- - - - - - - - - - - - - - - - - - - - - - - - - - E N D - - - - - - - - - - - - - - - - - - - - - - - - - -

IntroductionMonday 21st 9-10am

Turbulence theoryMonday 21st 11-12am

Measuring turbulenceMonday 28th 9-10am

Modelling turbulenceMonday 28th 11-12am

Marine Turbulence and Mixing

2. Turbulence theory

Dr. Matthew Palmer

matthew.palmer@noc.ac.uk

- Random, chaotic, irregular and unpredictable. Requires statistical representation.
- Vortical.
- 3-dimensional.
- Dissipative, always.
- Unsteady, unstable. Occurring over a broad spectrum of length and time scales.
- Diffusive. Promoting enhanced transfer by mixing.

- Turbulence is complex, chaotic and unstable
- It is therefore impossible to predict
- A convenient method of describing turbulence separates the flow u into the predictable mean part U and the turbulent part u’.
- We refer to this technique as Reynolds decomposition.

Osbourne Reynolds

1842 -1912

U

u = U + u’

W+w’

z

w

v

V+v’

Consider the momentum flux (unit area) in the x direction of a particle through area A at the velocity u, or U+u’.

y

U+u’

u

=

x

A

Momentum flux =

(mass(m-3) x velocity) x flux through A

r (u+u’).(u+u’).A

The mean force per unit area, or stress, in the x direction by flow u is,

and in the y and z direction,

r (U+u’).(V+v’).A

r (U+u’).(W+w’).A

and

but , so

Normal stresses

Symmetric

In the ocean, vertical gradients are much stronger than horizontal so we may disregard horizontal components of stress

The 9 cartesian Reynolds stress tensor

So we may now only consider txz and tyz or r u’w’ and r v’w’

u'

z

w'

x

Reynolds decomposition is also applicable to scalar quantities (temperature, salinity, density, nutrients etc.)

s = S + s’

s‘ = 0

But remember, turbulence is random, chaotic, broad spectrum and so difficult to measure. So we often need to parameterise the process of generating turbulence.

Consider how turbulent eddies interact.

Reynolds stress transfers energy from the horizontal to vertical and vortical turbulent motion.

txz = r u’w’

tyz = r v’w’

Sheared Flow

Due to its diffusive nature we may approximate these stresses to act in a similar way to molecular diffusivity but on larger scales (Bousinesq).

We may then parameterise the generation of turbulence by gradients in the mean flow.

1842-1929

Nz is the vertical eddy viscosity coefficient (m2s-1)

Remember that we may consider the turbulent properties of scalar quantities such as density or temperature in the same was as momentum.

s = S + s’

s‘ = 0

We may also approximate eddy diffusivity from molecular processes.

therfore

Kz is the vertical eddy diffusivity coefficient (m2s-1)

Which gives us the advection-diffusion equation for a scalar quantity:

Which represents the local rate of change of the scalar s in terms of horizontal advection by the mean flow U and vertical diffusion by the turbulent fluctuations within the water column.

We now have methods for quantifying complex turbulent processes by representing the statistical properties of turbulent flow and by considering them to behave similar to molecular processes,

within the equations of motion

and within the turbulent kinetic energy (E) budget,

Where P = production (+ve)

B = buoyant production (+ve or –ve)

e = dissipation (-ve)

In the absence of convection, there is TKE production is in balance with work against buoyancy and TKE dissipation.

e

Buoyant P

But there is a limiting factor!

Above a certain ratio of B/P turbulence will be suppressed.

Production

So we can define an expression to calculate the eddy diffusivity coefficient Kz.

Where

Where G ~0.2 (Osborn, 1980)

If velocity changes with depth in a stable, stratified flow, then the flow may become unstable providing that the shear flow is large enough.

The limiting condition for the development of turbulence is that the energy supply from the mean flow is greater than the energy demands of dissipation and mixing.

Turbulence is hungry!

Assuming that NzKz, then we may consider the relative stability as a competition between destabilising shear flow and stabilising buoyancy. The gradient Richardson number,

Where Rig ≤ ¼ somewhere within the flow instability may exist and disturbances may grow (Miles (1961) and Howard (1961) )

- Turbulent properties are chaotic so difficult to quantify.
- We have therefore represented turbulence in the EoM by approximation of its statistical properties.
- Using Nz and Kz to represent the viscous and diffusive nature of turbulence.
- Defined an expression for turbulent diffusion, Kz.
- Provided a method for quantifying the relative stability of the flow using Rig.

ADCPs are able to sample u fast enough to measure u’w’ and v’w’ and so we can directly calculate Reynolds stresses, eddy viscosity and TKE production……

…..Next week