In fluid dynamics, gravity waves are waves generated in a fluid medium or at the interface between two media when the force of gravity or buoyancy tries to restore equilibrium. An example of such an interface is that between the atmosphere and the ocean, which gives rise to wind waves.
A gravity wave results when fluid is displaced from a position of equilibrium. The restoration of the fluid to equilibrium will produce a movement of the fluid back and forth, called a wave orbit. Gravity waves on an air–sea interface of the ocean are called surface gravity waves (a type of surface wave), while gravity waves that are the body of the water (such as between parts of different densities) are called internal waves. Wind-generated waves on the water surface are examples of gravity waves, as are tsunamis, ocean tides, and the wakes of surface vessels.
The period of wind-generated gravity waves on the free surface of the Earth's ponds, lakes, seas and oceans are predominantly between 0.3 and 30 seconds (corresponding to frequencies between 3 Hz and .03 Hz). Shorter waves are also affected by surface tension and are called gravity–capillary waves and (if hardly influenced by gravity) capillary waves. Alternatively, so-called infragravity waves, which are due to subharmonic nonlinear wave interaction with the wind waves, have periods longer than the accompanying wind-generated waves.
See also: Undular bore. In the Earth's atmosphere, gravity waves are a mechanism that produce the transfer of momentum from the troposphere to the stratosphere and mesosphere. Gravity waves are generated in the troposphere by frontal systems or by airflow over mountains. At first, waves propagate through the atmosphere without appreciable change in mean velocity. But as the waves reach more rarefied (thin) air at higher altitudes, their amplitude increases, and nonlinear effects cause the waves to break, transferring their momentum to the mean flow. This transfer of momentum is responsible for the forcing of the many large-scale dynamical features of the atmosphere. For example, this momentum transfer is partly responsible for the driving of the Quasi-Biennial Oscillation, and in the mesosphere, it is thought to be the major driving force of the Semi-Annual Oscillation. Thus, this process plays a key role in the dynamics of the middle atmosphere.
The effect of gravity waves in clouds can look like altostratus undulatus clouds, and are sometimes confused with them, but the formation mechanism is different. Atmospheric gravity waves reaching ionosphere are responsible for the generation of traveling ionospheric disturbances and could be observed by radars. [1]
c
k
| c=\sqrt{ | g |
| k |
where g is the acceleration due to gravity. When surface tension is important, this is modified to
| c=\sqrt{ | g | + |
| k |
| \sigmak | |
| \rho |
where σ is the surface tension coefficient and ρ is the density.
The gravity wave represents a perturbation around a stationary state, in which there is no velocity. Thus, the perturbation introduced to the system is described by a velocity field of infinitesimally small amplitude,
(u'(x,z,t),w'(x,z,t)).
bf{u}'=(u'(x,z,t),w'(x,z,t))=(\psiz,-\psix),
where the subscripts indicate partial derivatives. In this derivation it suffices to work in two dimensions
\left(x,z\right)
\nabla x bf{u}'=0.
\nabla2\psi=0.
\psi\left(x,z,t\right)=eik\left(x-ct\right)\Psi\left(z\right),
where k is a spatial wavenumber. Thus, the problem reduces to solving the equation
\left(D2-k
| ||||
.
We work in a sea of infinite depth, so the boundary condition is at
\scriptstylez=-infty.
\scriptstylez=0
\scriptstylez=η,
\scriptstyleη
u=D\Psi=0,onz=-infty.
Hence,
\scriptstyle\Psi=Aek
\scriptstylez\in\left(-infty,η\right)
The free-surface condition: At the free surface
\scriptstylez=η\left(x,t\right)
| \partialη | +u' | |
| \partialt |
| \partialη | |
| \partialx |
=w'\left(η\right).
Linearizing, this is simply
| \partialη | |
| \partialt |
=w'\left(0\right),
where the velocity
\scriptstylew'\left(η\right)
\scriptstylez=0.
\scriptstylecη=\Psi
Pressure relation across the interface: For the case with surface tension, the pressure difference over the interface at
\scriptstylez=η
p\left(z=η\right)=-\sigma\kappa,
where σ is the surface tension and κ is the curvature of the interface, which in a linear approximation is
| 2η=η | |
| \kappa=\nabla | |
| xx |
.
Thus,
p\left(z=η\right)=-\sigmaηxx.
However, this condition refers to the total pressure (base+perturbed), thus
\left[P\left(η\right)+p'\left(0\right)\right]=-\sigmaηxx.
(As usual, The perturbed quantities can be linearized onto the surface z=0.) Using hydrostatic balance, in the form
\scriptstyleP=-\rhogz+Const.,
this becomes
p=gη\rho-\sigmaηxx, onz=0.
The perturbed pressures are evaluated in terms of streamfunctions, using the horizontal momentum equation of the linearised Euler equations for the perturbations,
| \partialu' | |
| \partialt |
=-
| 1 | |
| \rho |
| \partialp' | |
| \partialx |
to yield
\scriptstylep'=\rhocD\Psi.
Putting this last equation and the jump condition together,
c\rhoD\Psi=gη\rho-\sigmaηxx.
Substituting the second interfacial condition
\scriptstylecη=\Psi
\scriptstylec2\rhoD\Psi=g\Psi\rho+\sigmak2\Psi.
Using the solution
\scriptstyle\Psi=ek
| c=\sqrt{ | g | + |
| k |
| \sigmak | |
| \rho |
Since
\scriptstylec=\omega/k
\omega
\omega=\sqrt{gk}.
The group velocity of a wave (that is, the speed at which a wave packet travels) is given by
| c | ||||
|
,
and thus for a gravity wave,
| c | \sqrt{ | ||||
|
| g | |
| k |
The group velocity is one half the phase velocity. A wave in which the group and phase velocities differ is called dispersive.
Gravity waves traveling in shallow water (where the depth is much less than the wavelength), are nondispersive: the phase and group velocities are identical and independent of wavelength and frequency. When the water depth is h,
cp=cg=\sqrt{gh}.
See main article: Wind wave. Wind waves, as their name suggests, are generated by wind transferring energy from the atmosphere to the ocean's surface, and capillary-gravity waves play an essential role in this effect. There are two distinct mechanisms involved, called after their proponents, Phillips and Miles.
In the work of Phillips, the ocean surface is imagined to be initially flat (glassy), and a turbulent wind blows over the surface. When a flow is turbulent, one observes a randomly fluctuating velocity field superimposed on a mean flow (contrast with a laminar flow, in which the fluid motion is ordered and smooth). The fluctuating velocity field gives rise to fluctuating stresses (both tangential and normal) that act on the air-water interface. The normal stress, or fluctuating pressure acts as a forcing term (much like pushing a swing introduces a forcing term). If the frequency and wavenumber
\scriptstyle\left(\omega,k\right)
The air-water interface is now endowed with a surface roughness due to the capillary-gravity waves, and a second phase of wave growth takes place. A wave established on the surface either spontaneously as described above, or in laboratory conditions, interacts with the turbulent mean flow in a manner described by Miles. This is the so-called critical-layer mechanism. A critical layer forms at a height where the wave speed c equals the mean turbulent flow U. As the flow is turbulent, its mean profile is logarithmic, and its second derivative is thus negative. This is precisely the condition for the mean flow to impart its energy to the interface through the critical layer. This supply of energy to the interface is destabilizing and causes the amplitude of the wave on the interface to grow in time. As in other examples of linear instability, the growth rate of the disturbance in this phase is exponential in time.
This Miles–Phillips Mechanism process can continue until an equilibrium is reached, or until the wind stops transferring energy to the waves (i.e., blowing them along) or when they run out of ocean distance, also known as fetch length.