The shallowwater equations are a set of hyperbolic partial differential equations (or parabolic if viscous shear is considered) that describe the flow below a pressure surface in a fluid (sometimes, but not necessarily, a free surface).^{[1]} The shallowwater equations in unidirectional form are also called SaintVenant equations, after Adhémar Jean Claude Barré de SaintVenant (see the related section below).
The equations are derived^{[2]} from depthintegrating the Navier–Stokes equations, in the case where the horizontal length scale is much greater than the vertical length scale. Under this condition, conservation of mass implies that the vertical velocity scale of the fluid is small compared to the horizontal velocity scale. It can be shown from the momentum equation that vertical pressure gradients are nearly hydrostatic, and that horizontal pressure gradients are due to the displacement of the pressure surface, implying that the horizontal velocity field is constant throughout the depth of the fluid. Vertically integrating allows the vertical velocity to be removed from the equations. The shallowwater equations are thus derived.
While a vertical velocity term is not present in the shallowwater equations, note that this velocity is not necessarily zero. This is an important distinction because, for example, the vertical velocity cannot be zero when the floor changes depth, and thus if it were zero only flat floors would be usable with the shallowwater equations. Once a solution (i.e. the horizontal velocities and free surface displacement) has been found, the vertical velocity can be recovered via the continuity equation.
Situations in fluid dynamics where the horizontal length scale is much greater than the vertical length scale are common, so the shallowwater equations are widely applicable. They are used with Coriolis forces in atmospheric and oceanic modeling, as a simplification of the primitive equations of atmospheric flow.
Shallowwater equation models have only one vertical level, so they cannot directly encompass any factor that varies with height. However, in cases where the mean state is sufficiently simple, the vertical variations can be separated from the horizontal and several sets of shallowwater equations can describe the state.
The shallowwater equations are derived from equations of conservation of mass and conservation of linear momentum (the Navier–Stokes equations), which hold even when the assumptions of shallowwater break down, such as across a hydraulic jump. In the case of a horizontal bed, with negligible Coriolis forces, frictional and viscous forces, the shallowwater equations are:
Here η is the total fluid column height (instantaneous fluid depth as a function of x, y and t), and the 2D vector (u,v) is the fluid's horizontal flow velocity, averaged across the vertical column. Further g is acceleration due to gravity and ρ is the fluid density. The first equation is derived from mass conservation, the second two from momentum conservation.^{[3]}
Expanding the derivatives in the above using the product rule, the nonconservative form of the shallowwater equations is obtained. Since velocities are not subject to a fundamental conservation equation, the nonconservative forms do not hold across a shock or hydraulic jump. Also included are the appropriate terms for Coriolis, frictional and viscous forces, to obtain (for constant fluid density):
where
u  is the velocity in the x direction, or zonal velocity 
v  is the velocity in the y direction, or meridional velocity 
H  is the mean height of the horizontal pressure surface 
h  is the height deviation of the horizontal pressure surface from its mean height, where h: η(x, y, t) = H(x, y) + h(x, y, t) 
b  is the topographical height from a reference D, where b: H(x, y) = D + b(x,y) 
g  is the acceleration due to gravity 
f  is the Coriolis coefficient associated with the Coriolis force. On Earth, f is equal to 2Ω sin(φ), where Ω is the angular rotation rate of the Earth (π/12 radians/hour), and φ is the latitude 
k  is the viscous drag coefficient 
ν  is the kinematic viscosity 
It is often the case that the terms quadratic in u and v, which represent the effect of bulk advection, are small compared to the other terms. This is called geostrophic balance, and is equivalent to saying that the Rossby number is small. Assuming also that the wave height is very small compared to the mean height (h ≪ H), we have (without lateral viscous forces):
The onedimensional (1D) SaintVenant equations were derived by Adhémar Jean Claude Barré de SaintVenant, and are commonly used to model transient openchannel flow and surface runoff. They can be viewed as a contraction of the twodimensional (2D) shallowwater equations, which are also known as the twodimensional SaintVenant equations. The 1D SaintVenant equations contain to a certain extent the main characteristics of the channel crosssectional shape.
The 1D equations are used extensively in computer models such as TUFLOW, Mascaret (EDF), SIC (Irstea), HECRAS,^{[5]} SWMM5, ISIS,^{[5]} InfoWorks,^{[5]} Flood Modeller, SOBEK 1DFlow, MIKE 11,^{[5]} and MIKE SHE because they are significantly easier to solve than the full shallowwater equations. Common applications of the 1D SaintVenant equations include flood routing along rivers (including evaluation of measures to reduce the risks of flooding), dam break analysis, storm pulses in an open channel, as well as storm runoff in overland flow.
The system of partial differential equations which describe the 1D incompressible flow in an open channel of arbitrary cross section – as derived and posed by SaintVenant in his 1871 paper (equations 19 & 20) – is:^{[6]}

(1) 
and

(2) 
where x is the space coordinate along the channel axis, t denotes time, A(x,t) is the crosssectional area of the flow at location x, u(x,t) is the flow velocity, ζ(x,t) is the free surface elevation and τ(x,t) is the wall shear stress along the wetted perimeter P(x,t) of the cross section at x. Further ρ is the (constant) fluid density and g is the gravitational acceleration.
Closure of the hyperbolic system of equations (1)–(2) is obtained from the geometry of cross sections – by providing a functional relationship between the crosssectional area A and the surface elevation ζ at each position x. For example, for a rectangular cross section, with constant channel width B and channel bed elevation z_{b}, the cross sectional area is: A = B (ζ − z_{b}) = B h. The instantaneous water depth is h(x,t) = ζ(x,t) − z_{b}(x), with z_{b}(x) the bed level (i.e. elevation of the lowest point in the bed above datum, see the crosssection figure). For nonmoving channel walls the crosssectional area A in equation (1) can be written as:
The wall shear stress τ is dependent on the flow velocity u, they can be related by using e.g. the Darcy–Weisbach equation, Manning formula or Chézy formula.
Further, equation (1) is the continuity equation, expressing conservation of water volume for this incompressible homogeneous fluid. Equation (2) is the momentum equation, giving the balance between forces and momentum change rates.
The bed slope S(x), friction slope S_{f}(x, t) and hydraulic radius R(x, t) are defined as:
Consequently, the momentum equation (2) can be written as:^{[7]}

(3) 
The momentum equation (3) can also be cast in the socalled conservation form, through some algebraic manipulations on the SaintVenant equations, (1) and (3). In terms of the discharge Q = Au:^{[8]}

(4) 
where A, I_{1} and I_{2} are functions of the channel geometry, described in the terms of the channel width B(σ,x). Here σ is the height above the lowest point in the cross section at location x, see the crosssection figure. So σ is the height above the bed level z_{b}(x) (of the lowest point in the cross section):
Above – in the momentum equation (4) in conservation form – A, I_{1} and I_{2} are evaluated at σ = h(x,t). The term g I_{1} describes the hydrostatic force in a certain cross section. And, for a nonprismatic channel, g I_{2} gives the effects of geometry variations along the channel axis x.
In applications, depending on the problem at hand, there often is a preference for using either the momentum equation in nonconservation form, (2) or (3), or the conservation form (4). For instance in case of the description of hydraulic jumps, the conservation form is preferred since the momentum flux is continuous across the jump.
The SaintVenant equations (1)–(2) can be analysed using the method of characteristics.^{[9]}^{[10]}^{[11]}^{[12]} The two celerities dx/dt on the characteristic curves are:^{[8]}
The Froude number Fr = u / c determines whether the flow is subcritical (Fr < 1) or supercritical (Fr > 1).
For a rectangular and prismatic channel of constant width B, i.e. with A = B h and c = √gh, the Riemann invariants are:^{[9]}
The Riemann invariants and method of characteristics for a prismatic channel of arbitrary crosssection are described by Didenkulova & Pelinovsky (2011).^{[12]}
The characteristics and Riemann invariants provide important information on the behavior of the flow, as well as that they may be used in the process of obtaining (analytical or numerical) solutions.^{[13]}^{[14]}^{[15]}^{[16]}
The dynamic wave is the full onedimensional SaintVenant equation. It is numerically challenging to solve, but is valid for all channel flow scenarios. The dynamic wave is used for modeling transient storms in modeling programs including Mascaret (EDF), SIC (Irstea), HECRAS,^{[17]} InfoWorks_ICM,^{[18]} MIKE 11,^{[19]} Wash 123d^{[20]} and SWMM5.
In the order of increasing simplifications, by removing some terms of the full 1D SaintVenant equations (aka Dynamic wave equation), we get the also classical Diffusive wave equation and Kinematic wave equation.
For the diffusive wave it is assumed that the inertial terms are less than the gravity, friction, and pressure terms. The diffusive wave can therefore be more accurately described as a noninertia wave, and is written as:
The diffusive wave is valid when the inertial acceleration is much smaller than all other forms of acceleration, or in other words when there is primarily subcritical flow, with low Froude values. Models that use the diffusive wave assumption include MIKE SHE^{[21]} and LISFLOODFP.^{[22]} In the SIC (Irstea) software this options is also available, since the 2 inertia terms (or any of them) can be removed in option from the interface.
For the kinematic wave it is assumed that the flow is uniform, and that the friction slope is approximately equal to the slope of the channel. This simplifies the full SaintVenant equation to the kinematic wave:
The kinematic wave is valid when the change in wave height over distance and velocity over distance and time is negligible relative to the bed slope, e.g. for shallow flows over steep slopes.^{[23]} The kinematic wave is used in HECHMS.^{[24]}
This section possibly contains original research. (April 2018) 
The 1D SaintVenant momentum equation can be derived from the Navier–Stokes equations that describe fluid motion. The xcomponent of the Navier–Stokes equations – when expressed in Cartesian coordinates in the xdirection – can be written as:
where u is the velocity in the xdirection, v is the velocity in the ydirection, w is the velocity in the zdirection, t is time, p is the pressure, ρ is the density of water, ν is the kinematic viscosity, and f_{x} is the body force in the xdirection.
The local acceleration (a) can also be thought of as the "unsteady term" as this describes some change in velocity over time. The convective acceleration (b) is an acceleration caused by some change in velocity over position, for example the speeding up or slowing down of a fluid entering a constriction or an opening, respectively. Both these terms make up the inertia terms of the 1dimensional SaintVenant equation.
The pressure gradient term (c) describes how pressure changes with position, and since the pressure is assumed hydrostatic, this is the change in head over position. The friction term (d) accounts for losses in energy due to friction, while the gravity term (e) is the acceleration due to bed slope.
Shallowwater equations can be used to model Rossby and Kelvin waves in the atmosphere, rivers, lakes and oceans as well as gravity waves in a smaller domain (e.g. surface waves in a bath). In order for shallowwater equations to be valid, the wavelength of the phenomenon they are supposed to model has to be much larger than the depth of the basin where the phenomenon takes place. Somewhat smaller wavelengths can be handled by extending the shallowwater equations using the Boussinesq approximation to incorporate dispersion effects.^{[28]} Shallowwater equations are especially suitable to model tides which have very large length scales (over hundred of kilometers). For tidal motion, even a very deep ocean may be considered as shallow as its depth will always be much smaller than the tidal wavelength.
Shallowwater equations, in its nonlinear form, is an obvious candidate for modelling turbulence in the atmosphere and oceans, i.e. geophysical turbulence. An advantage of this, over Quasigeostrophic equations, is that it allows solutions like gravity waves, while also conserving energy and potential vorticity. However there are also some disadvantages as far as geophysical applications are concerned  it has a nonquadratic expression for total energy and a tendency for waves to become shock waves.^{[29]} Some alternate models have been proposed which prevent shock formation. One alternative is to modify the "pressure term" in the momentum equation, but it results in a complicated expression for kinetic energy.^{[30]} Another option is to modify the nonlinear terms in all equations, which gives a quadratic expression for kinetic energy, avoids shock formation, but conserves only linearized potential vorticity.^{[31]}