Airy Wave Theory 1: Wave Length and Celerity - CLAS Usersusers.clas.ufl.edu/.../GLY4734_Spring2014/S10_AiryWaveTheory.pptx.pdf · No single theory best describes the full range of

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Airy Wave Theory 1: Wave Length and Celerity

Wave Theories

Mathematical relationships to describe: (1)  the wave form, (2)  the water motion

(throughout the fluid column) and pressure in waves, and

(3) how (1) & (2) change with shoaling.

We’ll obtain expressions for the movement of water particles under passing waves - important to considerations of sediment transport --> coastal geomorphology.

No single theory best describes the full range of conditions found in nature!

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Linear (Airy) Wave Theory

Originates from Navier Stokes --> Euler Equations Works very well in deep water, but only applicable when L >> H, so it breaks down in shallow water. Solution is eta relationship: Wave Number: k = 2π/L Radian Frequency: σ = 2π/T

George Biddell Airy (1801-1892)

Water Surface Displacement Equation

What is the wave height? What is the wave period?

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Dispersion Equation: Convert to a general expression for Wave Celerity

Fundamental relationship in Airy Theory, which illustrates how waves segregate according to wave period: Substitute the relationships for radian frequency and wave number, respectively to get an equation for wavelength. Divide both sides by wave period to obtain an equation for wave speed (celerity). These are tough to solve, as L is on both sides of equality and contained within hyperbolic trigonometric function.

Effect of the Hyperbolic Trig Functions on Wave Celerity

What’s the relationship for celerity in deep water? What’s the relationship for celerity in shallow water?

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0 50 100 150 2000

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25

30

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45Airy Wave Celerity: General Expression, Deep− & Shallow− Approximations

Depth (m)

Cel

erity

(m/s

)

So the celerity illustrated is…

DWS, T=16 s

DWS, T=14 s

DWS, T=12 s

DWS, T=10 s

DWS, T=8 s

SWS, only depth dependent

Gen’l Soln., T=16 s

Gen’l Soln., T=14 s

Gen’l Soln., T=12 s

Gen’l Soln., T=10 s

Gen’l Soln., T=8 s

General Expression:

Deep-water expression:

Shallow-water expression:

Example 1 of Shallow Water Wave Speed - Tsunami

In Shallow Water

wave speed C = (gh)1/2

Deep Ocean Tsunami

C = (10m/s2*4000 m)1/2 ~200 m/s

~450 mph!

(Alaska to Hawaii in 4.7 hours)

How fast does a tsunami travel across the ocean? What classification is this wave? Deep water? Intermediate? Shallow water?

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Example 2 of Shallow Water Wave Speed – Tow-In Surfing

wave speed C = (gh)1/2

tow-in waves: H = ~8 m

C = (10 m/s2 * 10 m)1/2 ~ 10 m/s

~25 mph!

waves “surfable” by mortals:

C = (10 m/s2 * 2 m)1/2 ~ 4.4 m/s

~9 mph!

How fast does a Laird Hamilton surf?

Airy Wave Theory 2: Wave Orbitals and Energy

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Compilation of Airy Equations

Orbital Motion of Water Particles

Show code for this: /Users/pna/Work/mFiles/pna_library/wave_pna_codes/waveOrbVelDeep.m

Airy Wave Theory also predicts water particle orbital path trajectories. Orbital path divided by wave period provides the wave orbital velocity.

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0 10 20 30 40 50 60−0.8

−0.6

−0.4

−0.2

0

0.2

0.4

0.6

0.8

time (sec)

velo

city

(m/s

)

HorizontalVerticalTangential

Orbital Motion of Water Particles

Code for this: /Users/pna/Work/mFiles/pna_library/wave_pna_codes/waveOrbVelDeep.m

H=2m, T=10s, h=4000m

Where is the wave crest? The trough?

A B C D

Orbital Motion of Water Particles

Deep water (h>L/2): s=d=Hekz, circular orbits whose diameters decrease through water column to zero at h = L/2. At water surface, diameter of particle motion = wave height, H Intermediate water (h<L/2): elliptical orbits, whose size decrease downward through water column Shallow water: s=0, d=H/kh; ellipses flatten to horizontal motions; orbital diameter is constant from surface to bottom. Airy assumptions not valid in shallow water.

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Orbital Motion at the Bed in Shallow Water

The horizontal diameter at the bed simplifies to … And the maximum horizontal velocity at the bed, which relates conveniently to the shear stress, is

z

Total Energy =

Potential Energy + Kinetic Energy

€

E = Ep + Ek

€

=1L

ρgzdzdx−hη∫ +0

L∫1L

12ρ u2 + w2( )dzdx−h

η∫0L∫

=116

ρgH 2 +116

ρgH 2

=18ρgH 2

[dimensions] = M L L2 ; Units = joules/m2 or ergs/m2 L3 T2

Derivation of Wave Energy Density

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€

P =1T

Δp(x,z,t)[ ]udzdt−hη∫0

T∫

€

=18ρgH 2c 1

21+

2khsinh(2kh)

#

$ % &

' (

= Ecn

[dimensions] = M L L2 L L3 T2 T

= joules/sec/m = Watts/m

Deep Water n=1/2

Shallow Water n=1

Wave Energy Flux

Differs from energy density, as energy flux is equal to the energy density carried along by the moving waves. a.k.a. “Power per unit wave crest length”

[units]

Wave Groups

The expression Cn (sometimes written Cg) is known as the group celerity. In deep water, the first wave in a group decreases in height until it disappears and the second wave now becomes the leading wave (Figure). A new wave develops behind the last wave, thus maintaining the number of waves.

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Group velocity approx. cg = Δσ/ Δk ~ ∂σ/∂k

Deep Water: σ2 = gk cg = ∂σ/∂k = g/2σ = 1/2 c (use implicit differentiation)

Shallow Water: σ2 = ghk2 cg = ∂σ/∂k = (gh)1/2 = c (use implicit differentiation)

Individual Waves and Wave Group Velocity

!"

#$%

&+=

)2sinh(21

21

khkhn

The effect of the dispersion process is that, in deep water, the group of waves travels at a speed equal to ½ the speed of the individual waves in the group.* This is important in forecasting wave propagation and in particular the travel time of waves generated by a distant storm (hint for a problem on Assignment 3).

Stokes’s 2nd Order Wave Theory

Airy (linear) wave theory which makes use of a symmetric wave form, cannot predict the mass transport phenomena which arise from asymmetry that exists in the wave form in intermediate-to-shallow water. The wave form becomes distorted in shallower water. The crest narrows and the trough widens. Shoreward-directed horizontal velocity becomes higher under the wave crest than the offshore-directed velocity under the trough. Waves steepen and relative depth decreases, so that

these waves are no longer considered “small-amplitude”. Instead they are called “finite-amplitude”.

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Orbital Motion in Finite-Amplitude Wave Theory

Due to the asymmetry of the wave form, orbital paths are not closed. There is a net motion of the water particle in the direction of wave advance, called Stokes drift. Stokes drift is important because it provides a mechanism of sediment transport on beaches, independent of current-driven transport. Can divide drift distance by wave period to obtain drift velocity.

Shallow Water - Cnoidal and Solitary Wave Theories

Wave speed in shallow-water is influenced more by wave amplitude than water depth. The water particle motion is dominated by horizontal flows - vertical accelerations are small, and Stokes's theory becomes invalid. Mathematically complex formulations have emerged that predict shallow water wave forms well – Cnoidal and Solitary theory, which originates from the shallow water Boussinesq equation.

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Limits of Application