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In fluid dynamics, **dispersion** of water waves generally refers to frequency dispersion, which means that waves of different wavelengths travel at different phase speeds. Water waves, in this context, are waves propagating on the water surface, with gravity and surface tension as the restoring forces. As a result, water with a free surface is generally considered to be a dispersive medium.

In physics and engineering, **fluid dynamics** is a subdiscipline of fluid mechanics that describes the flow of fluids—liquids and gases. It has several subdisciplines, including aerodynamics and **hydrodynamics**. Fluid dynamics has a wide range of applications, including calculating forces and moments on aircraft, determining the mass flow rate of petroleum through pipelines, predicting weather patterns, understanding nebulae in interstellar space and modelling fission weapon detonation.

In the physical sciences and electrical engineering, **dispersion relations** describe the effect of dispersion in a medium on the properties of a wave traveling within that medium. A dispersion relation relates the wavelength or wavenumber of a wave to its frequency. From this relation the phase velocity and group velocity of the wave have convenient expressions which then determine the refractive index of the medium. More general than the geometry-dependent and material-dependent dispersion relations, there are the overarching Kramers–Kronig relations that describe the frequency dependence of wave propagation and attenuation.

In physics, mathematics, and related fields, a **wave** is a disturbance of one or more fields such that the field values oscillate repeatedly about a stable equilibrium (resting) value. If the relative amplitude of oscillation at different points in the field remains constant, the wave is said to be a standing wave. If the relative amplitude at different points in the field changes, the wave is said to be a traveling wave. Waves can only exist in fields when there is a force that tends to restore the field to equilibrium.

- Frequency dispersion for surface gravity waves
- Wave propagation and dispersion
- Phase velocity
- Group velocity
- Multi-component wave patterns
- Dispersion relation
- History
- Surface tension effects
- Interfacial waves
- Nonlinear effects
- Shallow water
- Deep water
- Waves on a mean current: Doppler shift
- See also
- Other articles on dispersion
- Dispersive water-wave models
- Notes
- References
- External links

For a certain water depth, surface gravity waves – i.e. waves occurring at the air–water interface and gravity as the only force restoring it to flatness – propagate faster with increasing wavelength. On the other hand, for a given (fixed) wavelength, gravity waves in deeper water have a larger phase speed than in shallower water.^{ [1] } In contrast with the behavior of gravity waves, capillary waves (i.e. only forced by surface tension) propagate faster for shorter wavelengths.

In physics, the **wavelength** is the **spatial period** of a periodic wave—the distance over which the wave's shape repeats. It is the distance between consecutive corresponding points of the same phase on the wave, such as two adjacent crests, troughs, or zero crossings, and is a characteristic of both traveling waves and standing waves, as well as other spatial wave patterns. The inverse of the wavelength is called the spatial frequency. Wavelength is commonly designated by the Greek letter *lambda* (λ). The term *wavelength* is also sometimes applied to modulated waves, and to the sinusoidal envelopes of modulated waves or waves formed by interference of several sinusoids.

The **shallow water equations** are a set of hyperbolic partial differential equations that describe the flow below a pressure surface in a fluid. The shallow water equations in unidirectional form are also called **Saint-Venant equations**, after Adhémar Jean Claude Barré de Saint-Venant.

A **capillary wave** is a wave traveling along the phase boundary of a fluid, whose dynamics and phase velocity are dominated by the effects of surface tension.

Besides frequency dispersion, water waves also exhibit amplitude dispersion. This is a nonlinear effect, by which waves of larger amplitude have a different phase speed from small-amplitude waves.

The **amplitude** of a periodic variable is a measure of its change over a single period. There are various definitions of amplitude, which are all functions of the magnitude of the difference between the variable's extreme values. In older texts the phase is sometimes called the amplitude.

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.

**Surface tension** is the tendency of fluid surfaces to shrink into the minimum surface area possible. Surface tension allows insects, usually denser than water, to float and slide on a water surface.

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] }

**Wave propagation** is any of the ways in which waves travel.

A **sine wave** or **sinusoid** is a mathematical curve that describes a smooth periodic oscillation. A sine wave is a continuous wave. It is named after the function sine, of which it is the graph. It occurs often in pure and applied mathematics, as well as physics, engineering, signal processing and many other fields. Its most basic form as a function of time (*t*) is:

The **elevation** of a geographic location is its height above or below a fixed reference point, most commonly a reference geoid, a mathematical model of the Earth's sea level as an equipotential gravitational surface . The term *elevation* is mainly used when referring to points on the Earth's surface, while *altitude* or *geopotential height* is used for points above the surface, such as an aircraft in flight or a spacecraft in orbit, and *depth* is used for points below the surface.

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] }

The **radian** is the SI unit for measuring angles, and is the standard unit of angular measure used in many areas of mathematics. The length of an arc of a unit circle is numerically equal to the measurement in radians of the angle that it subtends; one radian is just under 57.3 degrees. The unit was formerly an SI supplementary unit, but this category was abolished in 1995 and the radian is now considered an SI derived unit.

The **second** is the base unit of time in the International System of Units (SI), commonly understood and historically defined as ^{1}⁄_{86400} of a day – this factor derived from the division of the day first into 24 hours, then to 60 minutes and finally to 60 seconds each. Analog clocks and watches often have sixty tick marks on their faces, representing seconds, and a "second hand" to mark the passage of time in seconds. Digital clocks and watches often have a two-digit seconds counter. The second is also part of several other units of measurement like meters per second for velocity, meters per second per second for acceleration, and per second for frequency.

- with and

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 =*½*π*, - the downward zero-crossing at
*θ = π*and - the wave trough at
*θ = 1½ 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] }

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] }

or

an implicit equation with tanh denoting the hyperbolic tangent function.

An initial wave phase *θ = θ _{0}* propagates as a function of space and time. Its subsequent position is given by:

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

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] }

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.

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:

The dispersion characteristics for intermediate depth are given below.

More ... |
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In this deep-water case, the phase velocity is twice the group velocity. The red square overtakes two green circles, when moving from the left to the right of the figure. New waves seem to emerge at the back of a wave group, grow in amplitude until they are at the center of the group, and vanish at the wave group front. For gravity surface-waves, the water particle velocities are much smaller than the phase velocity, in most cases. |

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

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: *c _{g} = ½ c_{p}*.

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

More ... |
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For the shown case, a bichromatic group of gravity waves on the surface of deep water, the group velocity is half the phase velocity. In this example, there are 5⁄_{4} waves between two wave group nodes in space, while there are 11⁄_{2} waves between two wave group nodes in time. |

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:

So in deep water, with *c _{g} = ½ c_{p}*,

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] }

with:

*a*the wave amplitude of each frequency component in metres,*k*and_{1}*k*the wave number of each wave component, in radians per metre, and_{2}*ω*and_{1}*ω*the angular frequency of each wave component, in radians per second._{2}

Both *ω _{1}* and

- and

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

The part between square brackets is the slowly varying amplitude of the group, with group wave number *½ ( k _{1} − k_{2} )* and group angular frequency

Wave groups can only be discerned in case of a narrow-banded signal, with the wave-number difference *k _{1} − k_{2}* small compared to the mean wave number

More ... |
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For the three components respectively 22 (bottom), 25 (middle) and 29 (top) wavelengths fit in a horizontal domain of 2,000 meter length. The component with the shortest wavelength (top) propagates slowest. The wave amplitudes of the components are respectively 1, 2 and 1 meter. The differences in wavelength and phase speed of the components results in a changing pattern of wave groups, due to amplification where the components are in phase, and reduction where they are in anti-phase. |

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 *ω ^{2}* = [

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 > ½ λ ) | shallow water ( h < 0.05 λ ) | intermediate depth ( all λ and h ) |

dispersion relation | rad / s | ||||

phase velocity | m / s | ||||

group velocity | m / s | ||||

ratio | - | ||||

wavelength | m | for given period T, the solution of: |

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, *ω ^{2} = gh k^{2}*, was derived by Joseph Louis Lagrange.

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

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 *ω ^{2}* = Ω

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:

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:

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] }

- so

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:

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

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*.

- 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

- 1 2 Pond, S.; Pickard, G.L. (1978),
*Introductory dynamic oceanography*, Pergamon Press, pp. 170–174, ISBN 978-0-08-021614-0 - 1 2 3 4 See Lamb (1994), §229, pp. 366–369.
- ↑ See Whitham (1974), p.11.
- ↑ This dispersion relation is for a non-moving homogeneous medium, so in case of water waves for a constant water depth and no mean current.
- 1 2 3 See Phillips (1977), p. 37.
- ↑ See e.g. Dingemans (1997), p. 43.
- ↑ See Phillips (1977), p. 25.
- ↑ Reynolds, O. (1877), "On the rate of progression of groups of waves and the rate at which energy is transmitted by waves",
*Nature*,**16**(408): 343–44, Bibcode:1877Natur..16R.341., doi:10.1038/016341c0

Lord Rayleigh (J. W. Strutt) (1877), "On progressive waves",*Proceedings of the London Mathematical Society*,**9**: 21–26, doi:10.1112/plms/s1-9.1.21 Reprinted as Appendix in:*Theory of Sound***1**, MacMillan, 2nd revised edition, 1894. - ↑ See Lamb (1994), §237, pp. 382–384.
- 1 2 3 4 See Dingemans (1997), section 2.1.2, pp. 46–50.
- 1 2 3 See Lamb (1994), §236, pp. 380–382.
- ↑ Henderson, K. L.; Peregrine, D. H.; Dold, J. W. (1999), "Unsteady water wave modulations: fully nonlinear solutions and comparison with the nonlinear Schrödinger equation",
*Wave Motion*,**29**(4): 341–361, CiteSeerX 10.1.1.499.727 , doi:10.1016/S0165-2125(98)00045-6 - ↑ See Phillips (1977), p. 102.
- ↑ See Dean and Dalrymple (1991), page 65.
- ↑ See Craik (2004).
- ↑ See Lighthill (1978), pp. 224–225.
- ↑ Turner, J. S. (1979),
*Buoyancy effects in fluids*, Cambridge University Press, p. 18, ISBN 978-0521297264 - ↑ See e.g.: Craig, W.; Guyenne, P.; Hammack, J.; Henderson, D.; Sulem, C. (2006), "Solitary water wave interactions",
*Physics of Fluids*,**18**(57106): 057106–057106–25, Bibcode:2006PhFl...18e7106C, doi:10.1063/1.2205916 - ↑ See Lamb (1994), §250, pp. 417–420.
- ↑ See Phillips (1977), p. 24.

The **group velocity** of a wave is the velocity with which the overall envelope shape of the wave's amplitudes—known as the *modulation* or *envelope* of the wave—propagates through space.

The **phase velocity** of a wave is the rate at which the phase of the wave propagates in space. This is the velocity at which the phase of any one frequency component of the wave travels. For such a component, any given phase of the wave will appear to travel at the phase velocity. The phase velocity is given in terms of the wavelength λ (lambda) and time period T as

The **propagation constant** of a sinusoidal electromagnetic wave is a measure of the change undergone by the amplitude and phase of the wave as it propagates in a given direction. The quantity being measured can be the voltage, the current in a circuit, or a field vector such as electric field strength or flux density. The propagation constant itself measures the change per unit length, but it is otherwise dimensionless. In the context of two-port networks and their cascades, **propagation constant **measures the change undergone by the source quantity as it propagates from one port to the next.

A **wavenumber–frequency diagram** is a plot displaying the relationship between the wavenumber and the frequency of certain phenomena. Usually frequencies are placed on the vertical axis, while wavenumbers are placed on the horizontal axis.

**Synchrotron radiation** is the electromagnetic radiation emitted when charged particles are accelerated radially, e.g., when they are subject to an acceleration perpendicular to their velocity. It is produced, for example, in synchrotrons using bending magnets, undulators and/or wigglers. If the particle is non-relativistic, then the emission is called cyclotron emission. If, on the other hand, the particles are relativistic, sometimes referred to as ultrarelativistic, the emission is called synchrotron emission. Synchrotron radiation may be achieved artificially in synchrotrons or storage rings, or naturally by fast electrons moving through magnetic fields. The radiation produced in this way has a characteristic polarization and the frequencies generated can range over the entire electromagnetic spectrum which is also called continuum radiation.

In optics, **dispersion** is the phenomenon in which the phase velocity of a wave depends on its frequency. Media having this common property may be termed *dispersive media*. Sometimes the term ** chromatic dispersion** is used for specificity. Although the term is used in the field of optics to describe light and other electromagnetic waves, dispersion in the same sense can apply to any sort of wave motion such as acoustic dispersion in the case of sound and seismic waves, in gravity waves, and for telecommunication signals along transmission lines or optical fiber.

In physics, a **wave vector** is a vector which helps describe a wave. Like any vector, it has a magnitude and direction, both of which are important. Its magnitude is either the wavenumber or angular wavenumber of the wave, and its direction is ordinarily the direction of wave propagation.

**Internal waves** are gravity waves that oscillate within a fluid medium, rather than on its surface. To exist, the fluid must be stratified: the density must change with depth/height due to changes, for example, in temperature and/or salinity. If the density changes over a small vertical distance, the waves propagate horizontally like surface waves, but do so at slower speeds as determined by the density difference of the fluid below and above the interface. If the density changes continuously, the waves can propagate vertically as well as horizontally through the fluid.

**Atmospheric tides** are global-scale periodic oscillations of the atmosphere. In many ways they are analogous to ocean tides. Atmospheric tides can be excited by:

In fluid dynamics, a **Stokes wave** is a non-linear and periodic surface wave on an inviscid fluid layer of constant mean depth. This type of modelling has its origins in the mid 19th century when Sir George Stokes – using a perturbation series approach, now known as the **Stokes expansion** – obtained approximate solutions for non-linear wave motion.

In fluid dynamics, **wave shoaling** is the effect by which surface waves entering shallower water change in wave height. It is caused by the fact that the group velocity, which is also the wave-energy transport velocity, changes with water depth. Under stationary conditions, a decrease in transport speed must be compensated by an increase in energy density in order to maintain a constant energy flux. Shoaling waves will also exhibit a reduction in wavelength while the frequency remains constant.

In fluid dynamics, **Airy wave theory** gives a linearised description of the propagation of gravity waves on the surface of a homogeneous fluid layer. The theory assumes that the fluid layer has a uniform mean depth, and that the fluid flow is inviscid, incompressible and irrotational. This theory was first published, in correct form, by George Biddell Airy in the 19th century.

In fluid dynamics, the **mild-slope equation** describes the combined effects of diffraction and refraction for water waves propagating over bathymetry and due to lateral boundaries—like breakwaters and coastlines. It is an approximate model, deriving its name from being originally developed for wave propagation over mild slopes of the sea floor. The mild-slope equation is often used in coastal engineering to compute the wave-field changes near harbours and coasts.

In physics and engineering, the **envelope** of an oscillating signal is a smooth curve outlining its extremes. The envelope thus generalizes the concept of a constant amplitude. The figure illustrates a modulated sine wave varying between an upper and a lower envelope. The envelope function may be a function of time, space, angle, or indeed of any variable.

In optics, the **Fraunhofer diffraction equation** is used to model the diffraction of waves when the diffraction pattern is viewed at a long distance from the diffracting object, and also when it is viewed at the focal plane of an imaging lens.

In fluid dynamics, a **trochoidal wave** or **Gerstner wave** is an exact solution of the Euler equations for periodic surface gravity waves. It describes a progressive wave of permanent form on the surface of an incompressible fluid of infinite depth. The free surface of this wave solution is an inverted (upside-down) trochoid – with sharper crests and flat troughs. This wave solution was discovered by Gerstner in 1802, and rediscovered independently by Rankine in 1863.

- Craik, A.D.D. (2004), "The origins of water wave theory",
*Annual Review of Fluid Mechanics*,**36**: 1–28, Bibcode:2004AnRFM..36....1C, doi:10.1146/annurev.fluid.36.050802.122118 - Dean, R.G.; Dalrymple, R.A. (1991), "Water wave mechanics for engineers and scientists",
*Eos Transactions*, Advanced Series on Ocean Engineering,**2**(24): 490, Bibcode:1985EOSTr..66..490B, doi:10.1029/EO066i024p00490-06, ISBN 978-981-02-0420-4, OCLC 22907242 - Dingemans, M.W. (1997), "Water wave propagation over uneven bottoms",
*NASA Sti/Recon Technical Report N*, Advanced Series on Ocean Engineering,**13**: 25769, Bibcode:1985STIN...8525769K, ISBN 978-981-02-0427-3, OCLC 36126836 , 2 Parts, 967 pages. - Lamb, H. (1994),
*Hydrodynamics*(6th ed.), Cambridge University Press, ISBN 978-0-521-45868-9, OCLC 30070401 Originally published in 1879, the 6th extended edition appeared first in 1932. - Landau, L.D.; Lifshitz, E.M. (1987),
*Fluid Mechanics*, Course of theoretical physics,**6**(2nd ed.), Pergamon Press, ISBN 978-0-08-033932-0 - Lighthill, M.J. (1978),
*Waves in fluids*, Cambridge University Press, 504 pp, ISBN 978-0-521-29233-7, OCLC 2966533 - Phillips, O.M. (1977),
*The dynamics of the upper ocean*(2nd ed.), Cambridge University Press, ISBN 978-0-521-29801-8, OCLC 7319931 - Whitham, G. B. (1974),
*Linear and nonlinear waves*, Wiley-Interscience, ISBN 978-0-471-94090-6, OCLC 815118

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

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