Dispersion (water waves)

This section is about frequency dispersion for waves on a fluid layer forced by gravity, and according to linear theory. For surface tension effects on frequency dispersion, see surface tension effects in Airy wave theory and capillary wave.

 

The simplest propagating wave of unchanging form is a sine wave. A sine wave with water surface elevation η(x, t) is given by:^[2]

${\displaystyle \eta (x,t)=a\sin \left(\theta (x,t)\right),\,}$ 

where a is the amplitude (in metres) and θ = θ(x, t) is the phase function (in radians), depending on the horizontal position (x, in metres) and time (t, in seconds):^[3]

${\displaystyle \theta =2\pi \left({\frac {x}{\lambda }}-{\frac {t}{T}}\right)=kx-\omega t,}$  with ${\displaystyle k={\frac {2\pi }{\lambda }}}$  and ${\displaystyle \omega ={\frac {2\pi }{T}},}$ 

where:

• λ is the wavelength (in metres),
• T is the period (in seconds),
• k is the wavenumber (in radians per metre) and
• ω is the angular frequency (in radians per second).

Characteristic phases of a water wave are:

• the upward zero-crossing at θ = 0,
• the wave crest at θ = ⁠1/2⁠ π,
• the downward zero-crossing at θ = π and
• the wave trough at θ = ⁠3/2⁠ π.

A certain phase repeats itself after an integer m multiple of 2π: sin(θ) = sin(θ+m•2π).

Essential for water waves, and other wave phenomena in physics, is that free propagating waves of non-zero amplitude only exist when the angular frequency ω and wavenumber k (or equivalently the wavelength λ and period T ) satisfy a functional relationship: the frequency dispersion relation^[4][5]

${\displaystyle \omega ^{2}=\Omega ^{2}(k).\,}$ 

The dispersion relation has two solutions: ω = +Ω(k) and ω = −Ω(k), corresponding to waves travelling in the positive or negative x–direction. The dispersion relation will in general depend on several other parameters in addition to the wavenumber k. For gravity waves, according to linear theory, these are the acceleration by gravity g and the water depth h. The dispersion relation for these waves is:^[6][5]

an implicit equation with tanh denoting the hyperbolic tangent function.

An initial wave phase θ = θ₀ propagates as a function of space and time. Its subsequent position is given by:

${\displaystyle x={\frac {\lambda }{T}}\,t+{\frac {\lambda }{2\pi }}\,\theta _{0}={\frac {\omega }{k}}\,t+{\frac {\theta _{0}}{k}}.}$ 

This shows that the phase moves with the velocity:^[2]

${\displaystyle c_{p}={\frac {\lambda }{T}}={\frac {\omega }{k}}={\frac {\Omega (k)}{k}},}$ 

which is called the phase velocity.

A sinusoidal wave, of small surface-elevation amplitude and with a constant wavelength, propagates with the phase velocity, also called celerity or phase speed. While the phase velocity is a vector and has an associated direction, celerity or phase speed refer only to the magnitude of the phase velocity. According to linear theory for waves forced by gravity, the phase speed depends on the wavelength and the water depth. For a fixed water depth, long waves (with large wavelength) propagate faster than shorter waves.

In the left figure, it can be seen that shallow water waves, with wavelengths λ much larger than the water depth h, travel with the phase velocity^[2]

${\displaystyle c_{p}={\sqrt {gh}}\qquad \scriptstyle {\text{(shallow water),}}\,}$ 

with g the acceleration by gravity and c_p the phase speed. Since this shallow-water phase speed is independent of the wavelength, shallow water waves do not have frequency dispersion.

Using another normalization for the same frequency dispersion relation, the figure on the right shows that for a fixed wavelength λ the phase speed c_p increases with increasing water depth.^[1] Until, in deep water with water depth h larger than half the wavelength λ (so for h/λ > 0.5), the phase velocity c_p is independent of the water depth:^[2]

${\displaystyle c_{p}={\sqrt {\frac {g\lambda }{2\pi }}}={\frac {g}{2\pi }}T\qquad \scriptstyle {\text{(deep water),}}}$ 

with T the wave period (the reciprocal of the frequency f, T=1/f ). So in deep water the phase speed increases with the wavelength, and with the period.

Since the phase speed satisfies c_p = λ/T = λf, wavelength and period (or frequency) are related. For instance in deep water:

${\displaystyle \lambda ={\frac {g}{2\pi }}T^{2}\qquad \scriptstyle {\text{(deep water).}}}$ 

The dispersion characteristics for intermediate depth are given below.

 

Interference of two sinusoidal waves with slightly different wavelengths, but the same amplitude and propagation direction, results in a beat pattern, called a wave group. As can be seen in the animation, the group moves with a group velocity c_g different from the phase velocity c_p, due to frequency dispersion.

The group velocity is depicted by the red lines (marked B) in the two figures above. In shallow water, the group velocity is equal to the shallow-water phase velocity. This is because shallow water waves are not dispersive. In deep water, the group velocity is equal to half the phase velocity: {{math|c_g = ⁠1/2⁠ c_p.^[7]

The group velocity also turns out to be the energy transport velocity. This is the velocity with which the mean wave energy is transported horizontally in a narrow-band wave field.^[8][9]

In the case of a group velocity different from the phase velocity, a consequence is that the number of waves counted in a wave group is different when counted from a snapshot in space at a certain moment, from when counted in time from the measured surface elevation at a fixed position. Consider a wave group of length Λ_g and group duration of τ_g. The group velocity is:^[10]

${\displaystyle c_{g}={\frac {\Lambda _{g}}{\tau _{g}}}.}$ 

 

 

The number of waves in a wave group, measured in space at a certain moment is: Λ_g / λ. While measured at a fixed location in time, the number of waves in a group is: τ_g / T. So the ratio of the number of waves measured in space to those measured in time is:

${\displaystyle {\tfrac {\text{No. of waves in space}}{\text{No. of waves in time}}}={\frac {\Lambda _{g}/\lambda }{\tau _{g}/T}}={\frac {\Lambda _{g}}{\tau _{g}}}\cdot {\frac {T}{\lambda }}={\frac {c_{g}}{c_{p}}}.}$ 

So in deep water, with c_g = ⁠1/2⁠ c_p,^[11] a wave group has twice as many waves in time as it has in space.^[12]

The water surface elevation η(x,t), as a function of horizontal position x and time t, for a bichromatic wave group of full modulation can be mathematically formulated as:^[11]

${\displaystyle \eta =a\,\sin \left(k_{1}x-\omega _{1}t\right)+a\,\sin \left(k_{2}x-\omega _{2}t\right),}$ 

with:

• a the wave amplitude of each frequency component in metres,
• k₁ and k₂ the wave number of each wave component, in radians per metre, and
• ω₁ and ω₂ the angular frequency of each wave component, in radians per second.

Both ω₁ and k₁, as well as ω₂ and k₂, have to satisfy the dispersion relation:

${\displaystyle \omega _{1}^{2}=\Omega ^{2}(k_{1})\,}$  and ${\displaystyle \omega _{2}^{2}=\Omega ^{2}(k_{2}).\,}$ 

Using trigonometric identities, the surface elevation is written as:^[10]

${\displaystyle \eta =\left[2\,a\,\cos \left({\frac {k_{1}-k_{2}}{2}}x-{\frac {\omega _{1}-\omega _{2}}{2}}t\right)\right]\;\cdot \;\sin \left({\frac {k_{1}+k_{2}}{2}}x-{\frac {\omega _{1}+\omega _{2}}{2}}t\right).}$ 

The part between square brackets is the slowly varying amplitude of the group, with group wave number ⁠1/2⁠ ( k₁ − k₂ ) and group angular frequency ⁠1/2⁠ ( ω₁ − ω₂ ). As a result, the group velocity is, for the limit k₁ → k₂ :^[10][11]

${\displaystyle c_{g}=\lim _{k_{1}\,\to \,k_{2}}{\frac {\omega _{1}-\omega _{2}}{k_{1}-k_{2}}}=\lim _{k_{1}\,\to \,k_{2}}{\frac {\Omega (k_{1})-\Omega (k_{2})}{k_{1}-k_{2}}}={\frac {{\text{d}}\Omega (k)}{{\text{d}}k}}.}$ 

Wave groups can only be discerned in case of a narrow-banded signal, with the wave-number difference k₁ − k₂ small compared to the mean wave number ⁠1/2⁠ (k₁ + k₂).

 

The effect of frequency dispersion is that the waves travel as a function of wavelength, so that spatial and temporal phase properties of the propagating wave are constantly changing. For example, under the action of gravity, water waves with a longer wavelength travel faster than those with a shorter wavelength.

While two superimposed sinusoidal waves, called a bichromatic wave, have an envelope which travels unchanged, three or more sinusoidal wave components result in a changing pattern of the waves and their envelope. A sea state – that is: real waves on the sea or ocean – can be described as a superposition of many sinusoidal waves with different wavelengths, amplitudes, initial phases and propagation directions. Each of these components travels with its own phase velocity, in accordance with the dispersion relation. The statistics of such a surface can be described by its power spectrum.^[13]

In the table below, the dispersion relation ω² = [Ω(k)]² between angular frequency ω = 2π / T and wave number k = 2π / λ is given, as well as the phase and group speeds.^[10]

Frequency dispersion of gravity waves on the surface of deep water, shallow water and at intermediate depth, according to linear wave theory
quantity	symbol	units	deep water ( h > ⁠1/2⁠ λ )	shallow water ( h < 0.05 λ )	intermediate depth ( all λ and h )
dispersion relation	${\displaystyle \displaystyle \Omega (k)}$	rad / s	${\displaystyle {\sqrt {gk}}={\sqrt {\frac {2\pi \,g}{\lambda }}}}$	${\displaystyle k{\sqrt {gh}}={\frac {2\pi }{\lambda }}{\sqrt {gh}}}$	${\displaystyle {\begin{aligned}&{\sqrt {gk\,\tanh \left(kh\right)}}\,\\[1.2ex]&={\sqrt {{\frac {2\pi g}{\lambda }}\tanh \left({\frac {2\pi h}{\lambda }}\right)}}\,\end{aligned}}}$
phase velocity	${\displaystyle \displaystyle c_{p}={\frac {\lambda }{T}}={\frac {\omega }{k}}}$	m / s	${\displaystyle {\sqrt {\frac {g}{k}}}={\frac {g}{\omega }}={\frac {g}{2\pi }}T}$	${\displaystyle {\sqrt {gh}}}$	${\displaystyle {\sqrt {{\frac {g}{k}}\tanh \left(kh\right)}}}$
group velocity	${\displaystyle \displaystyle c_{g}={\frac {\partial \Omega }{\partial k}}}$	m / s	${\displaystyle {\frac {1}{2}}{\sqrt {\frac {g}{k}}}={\frac {1}{2}}{\frac {g}{\omega }}={\frac {g}{4\pi }}T}$	${\displaystyle {\sqrt {gh}}}$	${\displaystyle {\frac {1}{2}}c_{p}\left(1+{\frac {2kh}{\sinh \left(2kh\right)}}\right)}$
ratio	${\displaystyle \displaystyle {\frac {c_{g}}{c_{p}}}}$	-	${\displaystyle \displaystyle {\frac {1}{2}}}$	${\displaystyle \displaystyle 1}$	${\displaystyle {\frac {1}{2}}\left(1+{\frac {2kh}{\sinh \left(2kh\right)}}\right)}$
wavelength	${\displaystyle \displaystyle \lambda }$	m	${\displaystyle {\frac {g}{2\pi }}T^{2}}$	${\displaystyle T{\sqrt {gh}}}$	for given period T, the solution of:   ${\displaystyle \displaystyle \left({\frac {2\pi }{T}}\right)^{2}={\frac {2\pi g}{\lambda }}\tanh \left({\frac {2\pi h}{\lambda }}\right)}$

Deep water corresponds with water depths larger than half the wavelength, which is the common situation in the ocean. In deep water, longer period waves propagate faster and transport their energy faster. The deep-water group velocity is half the phase velocity. In shallow water, for wavelengths larger than twenty times the water depth,^[14] as found quite often near the coast, the group velocity is equal to the phase velocity.

The full linear dispersion relation was first found by Pierre-Simon Laplace, although there were some errors in his solution for the linear wave problem. The complete theory for linear water waves, including dispersion, was derived by George Biddell Airy and published in about 1840. A similar equation was also found by Philip Kelland at around the same time (but making some mistakes in his derivation of the wave theory).^[15]

The shallow water (with small h / λ) limit, ω² = gh k², was derived by Joseph Louis Lagrange.

 

In case of gravity–capillary waves, where surface tension affects the waves, the dispersion relation becomes:^[5]

${\displaystyle \omega ^{2}=\left(gk+{\frac {\sigma }{\rho }}k^{3}\right)\tanh(kh),}$ 

with σ the surface tension (in N/m).

For a water–air interface (with σ = 0.074 N/m and ρ = 1000 kg/m³) the waves can be approximated as pure capillary waves – dominated by surface-tension effects – for wavelengths less than 0.4 cm (0.2 in). For wavelengths above 7 cm (3 in) the waves are to good approximation pure surface gravity waves with very little surface-tension effects.^[16]

 

For two homogeneous layers of fluids, of mean thickness h below the interface and h′ above – under the action of gravity and bounded above and below by horizontal rigid walls – the dispersion relationship ω² = Ω²(k) for gravity waves is provided by:^[17]

${\displaystyle \Omega ^{2}(k)={\frac {g\,k(\rho -\rho ')}{\rho \,\coth(kh)+\rho '\,\coth(kh')}},}$ 

where again ρ and ρ′ are the densities below and above the interface, while coth is the hyperbolic cotangent function. For the case ρ′ is zero this reduces to the dispersion relation of surface gravity waves on water of finite depth h.

When the depth of the two fluid layers becomes very large (h→∞, h′→∞), the hyperbolic cotangents in the above formula approaches the value of one. Then:

${\displaystyle \Omega ^{2}(k)={\frac {\rho -\rho '}{\rho +\rho '}}\,g\,k.}$ 

Amplitude dispersion effects appear for instance in the solitary wave: a single hump of water traveling with constant velocity in shallow water with a horizontal bed. Note that solitary waves are near-solitons, but not exactly – after the interaction of two (colliding or overtaking) solitary waves, they have changed a bit in amplitude and an oscillatory residual is left behind.^[18] The single soliton solution of the Korteweg–de Vries equation, of wave height H in water depth h far away from the wave crest, travels with the velocity:

${\displaystyle c_{p}=c_{g}={\sqrt {g(h+H)}}.}$ 

So for this nonlinear gravity wave it is the total water depth under the wave crest that determines the speed, with higher waves traveling faster than lower waves. Note that solitary wave solutions only exist for positive values of H, solitary gravity waves of depression do not exist.

The linear dispersion relation – unaffected by wave amplitude – is for nonlinear waves also correct at the second order of the perturbation theory expansion, with the orders in terms of the wave steepness k a (where a is wave amplitude). To the third order, and for deep water, the dispersion relation is^[19]

${\displaystyle \omega ^{2}=gk\left[1+(ka)^{2}\right],}$    so   ${\displaystyle c_{p}={\sqrt {\frac {g}{k}}}\,\left[1+{\tfrac {1}{2}}\,(ka)^{2}\right]+{\mathcal {O}}\left((ka)^{4}\right).}$ 

This implies that large waves travel faster than small ones of the same frequency. This is only noticeable when the wave steepness k a is large.

Water waves on a mean flow (so a wave in a moving medium) experience a Doppler shift. Suppose the dispersion relation for a non-moving medium is:

${\displaystyle \omega ^{2}=\Omega ^{2}(k),\,}$ 

with k the wavenumber. Then for a medium with mean velocity vector V, the dispersion relationship with Doppler shift becomes:^[20]

${\displaystyle \left(\omega -\mathbf {k} \cdot \mathbf {V} \right)^{2}=\Omega ^{2}(k),}$ 

where k is the wavenumber vector, related to k as: k = |k|. The dot product k•V is equal to: k•V = kV cos α, with V the length of the mean velocity vector V: V = |V|. And α the angle between the wave propagation direction and the mean flow direction. For waves and current in the same direction, k•V=kV.

• Dispersive partial differential equation
• Capillary wave

• Airy wave theory
• Benjamin–Bona–Mahony equation
• Boussinesq approximation (water waves)
• Cnoidal wave
• Camassa–Holm equation
• Davey–Stewartson equation
• Kadomtsev–Petviashvili equation (also known as KP equation)
• Korteweg–de Vries equation (also known as KdV equation)
• Luke's variational principle
• Nonlinear Schrödinger equation
• Shallow water equations
• Stokes' wave theory
• Trochoidal wave
• Wave turbulence
• Whitham equation

• Mathematical aspects of dispersive waves are discussed on the Dispersive Wiki.