# 1-D Saint-Venant equation

Output from a shallow-water equation model of water in a bathtub. The water experiences five splashes which generate surface gravity waves that propagate away from the splash locations and reflect off the bathtub walls.

The shallow-water 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 shallow-water equations in unidirectional form are also called Saint-Venant equations, after Adhémar Jean Claude Barré de Saint-Venant (see the related section below).

The equations are derived[2] from depth-integrating 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 shallow-water equations are thus derived.

While a vertical velocity term is not present in the shallow-water 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 shallow-water 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 shallow-water 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.

Shallow-water 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 shallow-water equations can describe the state.

## Equations[]

### Conservative form[]

The shallow-water 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 shallow-water break down, such as across a hydraulic jump. In the case of a horizontal bed, with negligible Coriolis forces, frictional and viscous forces, the shallow-water equations are:

{\displaystyle {\begin{aligned}{\frac {\partial (\rho \eta )}{\partial t}}&+{\frac {\partial (\rho \eta u)}{\partial x}}+{\frac {\partial (\rho \eta v)}{\partial y}}=0,\\[3pt]{\frac {\partial (\rho \eta u)}{\partial t}}&+{\frac {\partial }{\partial x}}\left(\rho \eta u^{2}+{\frac {1}{2}}\rho g\eta ^{2}\right)+{\frac {\partial (\rho \eta uv)}{\partial y}}=0,\\[3pt]{\frac {\partial (\rho \eta v)}{\partial t}}&+{\frac {\partial (\rho \eta uv)}{\partial x}}+{\frac {\partial }{\partial y}}\left(\rho \eta v^{2}+{\frac {1}{2}}\rho g\eta ^{2}\right)=0.\end{aligned}}}

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]

### Non-conservative form[]

Expanding the derivatives in the above using the product rule, the non-conservative form of the shallow-water equations is obtained. Since velocities are not subject to a fundamental conservation equation, the non-conservative 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):

{\displaystyle {\begin{aligned}{\frac {\partial h}{\partial t}}&+{\frac {\partial }{\partial x}}{\Bigl (}(H+h)u{\Bigr )}+{\frac {\partial }{\partial y}}{\Bigl (}(H+h)v{\Bigr )}=0,\\[3pt]{\frac {\partial u}{\partial t}}&+u{\frac {\partial u}{\partial x}}+v{\frac {\partial u}{\partial y}}-fv=-g{\frac {\partial h}{\partial x}}-bu+\nu \left({\frac {\partial ^{2}u}{\partial x^{2}}}+{\frac {\partial ^{2}u}{\partial y^{2}}}\right),\\[3pt]{\frac {\partial v}{\partial t}}&+u{\frac {\partial v}{\partial x}}+v{\frac {\partial v}{\partial y}}+fu=-g{\frac {\partial h}{\partial y}}-bv+\nu \left({\frac {\partial ^{2}v}{\partial x^{2}}}+{\frac {\partial ^{2}v}{\partial y^{2}}}\right),\end{aligned}}}

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 height deviation of the horizontal pressure surface from its mean height H: η = H + h H is the mean height of the horizontal pressure surface 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 b is the viscous drag coefficient ν is the kinematic viscosity
Animation of the linearized shallow-water equations for a rectangular basin, without friction and Coriolis force. The water experiences a splash which generates surface gravity waves that propagate away from the splash location and reflect off the basin walls. The animation is created using the exact solution of Carrier and Yeh (2005) for axisymmetrical waves.[4]

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 (hH), we have (without lateral viscous forces):

{\displaystyle {\begin{aligned}{\frac {\partial h}{\partial t}}&+H\left({\frac {\partial u}{\partial x}}+{\frac {\partial v}{\partial y}}\right)=0,\\[3pt]{\frac {\partial u}{\partial t}}&-fv=-g{\frac {\partial h}{\partial x}}-bu,\\[3pt]{\frac {\partial v}{\partial t}}&+fu=-g{\frac {\partial h}{\partial y}}-bv.\end{aligned}}}

## One-dimensional Saint-Venant equations[]

The one-dimensional (1-D) Saint-Venant equations were derived by Adhémar Jean Claude Barré de Saint-Venant, and are commonly used to model transient open-channel flow and surface runoff. They can be viewed as a contraction of the two-dimensional (2-D) shallow-water equations, which are also known as the two-dimensional Saint-Venant equations. The 1-D Saint-Venant equations contain to a certain extent the main characteristics of the channel cross-sectional shape.

The 1-D equations are used extensively in computer models such as TUFLOW, Mascaret (EDF), SIC (Irstea), HEC-RAS,[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 shallow-water equations. Common applications of the 1-D Saint-Venant 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.

### Equations[]

Cross section of the open channel.

The system of partial differential equations which describe the 1-D incompressible flow in an open channel of arbitrary cross section – as derived and posed by Saint-Venant in his 1871 paper (equations 19 & 20) – is:[6]

${\displaystyle {\frac {\partial A}{\partial t}}+{\frac {\partial \left(Au\right)}{\partial x}}=0}$   and

(1)

${\displaystyle {\frac {\partial u}{\partial t}}+u\,{\frac {\partial u}{\partial x}}+g\,{\frac {\partial \zeta }{\partial x}}=-{\frac {P}{A}}\,{\frac {\tau }{\rho }},}$

(2)

where x is the space coordinate along the channel axis, t denotes time, A(x,t) is the cross-sectional 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 cross-sectional 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 zb, the cross sectional area is: A = B (ζ − zb) = B h. The instantaneous water depth is h(x,t) = ζ(x,t) − zb(x), with zb(x) the bed level (i.e. elevation of the lowest point in the bed above datum, see the cross-section figure). For non-moving channel walls the cross-sectional area A in equation (1) can be written as:

${\displaystyle A(x,t)=\int _{0}^{h(x,t)}b(x,h')\;{\mbox{d}}h',}$

with b(x,h) the effective width of the channel cross section at location x when the fluid depth is h – so b(x,h) = B(x) for rectangular channels.[7]

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 Sf(x,t) and hydraulic radius R(x,t) are defined as:

${\displaystyle S=-{\frac {\mathrm {d} z_{\mathrm {b} }}{\mathrm {d} x}},}$   ${\displaystyle S_{\mathrm {f} }={\frac {\tau }{\rho gR}}}$   and   ${\displaystyle R={\frac {A}{P}}.}$

Consequently, the momentum equation (2) can be written as:[7]

${\displaystyle {\frac {\partial u}{\partial t}}+u\,{\frac {\partial u}{\partial x}}+g\,{\frac {\partial h}{\partial x}}+g\,\left(S_{\mathrm {f} }-S\right)=0.}$

(3)

### Conservation of momentum[]

The momentum equation (3) can also be cast in the so-called conservation form, through some algebraic manipulations on the Saint-Venant equations, (1) and (3). In terms of the discharge Q = Au:[8]

${\displaystyle {\frac {\partial Q}{\partial t}}+{\frac {\partial }{\partial x}}\left({\frac {Q^{2}}{A}}+g\,I_{1}\right)+g\,A\,\left(S_{f}-S\right)-g\,I_{2}=0,}$

(4)

where A, I1 and I2 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 cross-section figure. So σ is the height above the bed level zb(x) (of the lowest point in the cross section):

{\displaystyle {\begin{aligned}A(\sigma ,x)&=\int _{0}^{\sigma }B(\sigma ^{\prime },x)\;\mathrm {d} \sigma ^{\prime },\\I_{1}(\sigma ,x)&=\int _{0}^{\sigma }(\sigma -\sigma ^{\prime })\,B(\sigma ^{\prime },x)\;\mathrm {d} \sigma ^{\prime }\qquad {\text{and}}\\I_{2}(\sigma ,x)&=\int _{0}^{\sigma }(\sigma -\sigma ^{\prime })\,{\frac {\partial B(\sigma ^{\prime },x)}{\partial x}}\;\mathrm {d} \sigma ^{\prime }.\end{aligned}}}

Above – in the momentum equation (4) in conservation form – A, I1 and I2 are evaluated at σ = h(x,t). The term g I1 describes the hydrostatic force in a certain cross section. And, for a non-prismatic channel, g I2 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 non-conservation 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.

### Characteristics[]

Characteristics, domain of dependence and region of influence, associated with location P = (xP,tP) in space x and time t.

The Saint-Venant 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]

${\displaystyle {\frac {\mathrm {d} x}{\mathrm {d} t}}=u\pm c,}$   with   ${\displaystyle c={\sqrt {\frac {gA}{B}}}.}$

The Froude number F = |u| / c determines whether the flow is subcritical (F < 1) or supercritical (F > 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]

${\displaystyle r_{+}=u+2{\sqrt {gh}}}$   and   ${\displaystyle r_{-}=u-2{\sqrt {gh}},}$

so the equations in characteristic form are:[9]

{\displaystyle {\begin{aligned}&{\frac {\mathrm {d} }{\mathrm {d} t}}\left(u+2{\sqrt {gh}}\right)=g\left(S-S_{f}\right)&&{\text{along}}\quad {\frac {\mathrm {d} x}{\mathrm {d} t}}=u+{\sqrt {gh}}\quad {\text{and}}\\&{\frac {\mathrm {d} }{\mathrm {d} t}}\left(u-2{\sqrt {gh}}\right)=g\left(S-S_{f}\right)&&{\text{along}}\quad {\frac {\mathrm {d} x}{\mathrm {d} t}}=u-{\sqrt {gh}}.\end{aligned}}}

The Riemann invariants and method of characteristics for a prismatic channel of arbitrary cross-section 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]

### Derived modelling[]

#### Dynamic wave[]

The dynamic wave is the full one-dimensional Saint-Venant 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), HEC-RAS,[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 Saint-Venant equations (aka Dynamic wave equation), we get the also classical Diffusive wave equation and Kinematic wave equation.

#### Diffusive wave[]

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 non-inertia wave, and is written as:

${\displaystyle g{\frac {\partial h}{\partial x}}+g(S_{f}-S)=0.}$

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 LISFLOOD-FP.[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.

#### Kinematic wave[]

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 Saint-Venant equation to the kinematic wave:

${\displaystyle S_{f}-S=0.}$

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 HEC-HMS.[24]

### Derivation from Navier–Stokes equations[]

The 1-D Saint-Venant momentum equation can be derived from the Navier–Stokes equations that describe fluid motion. The x-component of the Navier–Stokes equations – when expressed in Cartesian coordinates in the x-direction – can be written as:

${\displaystyle {\frac {\partial u}{\partial t}}+u{\frac {\partial u}{\partial x}}+v{\frac {\partial u}{\partial y}}+w{\frac {\partial u}{\partial z}}=-{\frac {\partial p}{\partial x}}{\frac {1}{\rho }}+\nu \left({\frac {\partial ^{2}u}{\partial x^{2}}}+{\frac {\partial ^{2}u}{\partial y^{2}}}+{\frac {\partial ^{2}u}{\partial z^{2}}}\right)+f_{x},}$

where u is the velocity in the x-direction, v is the velocity in the y-direction, w is the velocity in the z-direction, t is time, p is the pressure, ρ is the density of water, ν is the kinematic viscosity, and fx is the body force in the x-direction.

 1 If it is assumed that friction is taken into account as a body force, then ${\displaystyle \nu }$ can be assumed as zero so: ${\displaystyle \nu \left({\frac {\partial ^{2}u}{\partial x^{2}}}+{\frac {\partial ^{2}u}{\partial y^{2}}}+{\frac {\partial ^{2}u}{\partial z^{2}}}\right)=0.}$ 2 Assuming one-dimensional flow in the x-direction it follows that:[25] ${\displaystyle v{\frac {\partial u}{\partial y}}+w{\frac {\partial u}{\partial z}}=0}$ 3 Assuming also that the pressure distribution is approximately hydrostatic it follows that:[25] ${\displaystyle p=\rho gh}$ or in differential form: ${\displaystyle \partial p=\rho g(\partial h).}$ And when these assumptions are applied to the x-component of the Navier–Stokes equations: ${\displaystyle -{\frac {\partial p}{\partial x}}{\frac {1}{\rho }}=-{\frac {1}{\rho }}{\frac {\rho g\left(\partial h\right)}{\partial x}}=-g{\frac {\partial h}{\partial x}}.}$ 4 There are 2 body forces acting on the channel fluid, namely, gravity and friction: ${\displaystyle f_{x}=f_{x,g}+f_{x,f}}$ where fx,g is the body force due to gravity and fx,f is the body force due to friction. 5 fx,g can be calculated using basic physics and trigonometry:[26] ${\displaystyle F_{g}=(\sin \theta )gM}$ where Fg is the force of gravity in the x-direction, θ is the angle, and M is the mass. Figure 1: Diagram of block moving down an inclined plane. The expression for sin θ can be simplified using trigonometry as: ${\displaystyle \sin \theta ={\frac {\text{opp}}{\text{hyp}}}.}$ For small θ (reasonable for almost all streams) it can be assumed that: ${\displaystyle \sin \theta =\tan \theta ={\frac {\text{opp}}{\text{adj}}}=S}$ and given that fx represents a force per unit mass, the expression becomes: ${\displaystyle f_{x,g}=gS.}$ 6 Assuming the energy grade line is not the same as the channel slope, and for a reach of consistent slope there is a consistent friction loss, it follows that:[27] ${\displaystyle f_{x,f}=S_{f}g.}$ 7 All of these assumptions combined arrives at the 1-dimensional Saint-Venant equation in the x-direction: ${\displaystyle {\frac {\partial u}{\partial t}}+u{\frac {\partial u}{\partial x}}+g{\frac {\partial h}{\partial x}}+g(S_{f}-S)=0,}$ ${\displaystyle (a)\quad \ \ (b)\quad \ \ \ (c)\qquad \ \ \ (d)\quad (e)\ }$ where (a) is the local acceleration term, (b) is the convective acceleration term, (c) is the pressure gradient term, (d) is the friction term, and (e) is the gravity term.
Terms

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 1-dimensional Saint-Venant 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.

## Wave modelling by shallow-water equations[]

Shallow-water 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 shallow-water 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 shallow-water equations using the Boussinesq approximation to incorporate dispersion effects.[28] Shallow-water 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.

Tsunami generation and propagation, as computed with the shallow-water equations (red line; without frequency dispersion)), and with a Boussinesq-type model (blue line; with frequency dispersion). Observe that the Boussinesq-type model (blue line) forms a soliton with an oscillatory tail staying behind. The shallow-water equations (red line) form a steep front, which will lead to bore formation, later on. The water depth is 100 meters.

## Turbulence modelling using non-linear shallow-water equations[]

A snapshot from simulation of shallow-water equations in which shock waves are present

Shallow-water equations, in its non-linear form, is an obvious candidate for modelling turbulence in the atmosphere and oceans, i.e. geophysical turbulence. An advantage of this, over Quasi-geostrophic 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 non-quadratic 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 non-linear terms in all equations, which gives a quadratic expression for kinetic energy, avoids shock formation, but conserves only linearized potential vorticity.[31]

## Notes[]

1. ^ Vreugdenhil, C.B. (1986). Numerical Methods for Shallow-Water Flow. Water Science and Technology Library. 13. Springer, Dordrecht. p. 262. doi:10.1007/978-94-015-8354-1. ISBN 978-90-481-4472-3.
2. ^ "The Shallow Water Equations" (PDF). Retrieved 2010-01-22.
3. ^ Clint Dawson and Christopher M. Mirabito (2008). "The Shallow Water Equations" (PDF). Retrieved 2013-03-28.
4. ^ Carrier, G. F.; Yeh, H. (2005), "Tsunami propagation from a finite source", Computer Modeling in Engineering & Sciences, 10 (2): 113–122, doi:10.3970/cmes.2005.010.113
5. ^ a b c d S. Néelz; G Pender (2009). "Desktop review of 2D hydraulic modelling packages". Joint Environment Agency/Defra Flood and Coastal Erosion Risk Management Research and Development Programme (Science Report: SC080035): 5. Retrieved 2 December 2016.
6. ^ Saint-Venant, A.J.C. Barré de (1871), "Théorie du mouvement non permanent des eaux, avec application aux crues des rivières et a l'introduction de marées dans leurs lits", Comptes Rendus de l'Académie des Sciences, 73: 147–154 and 237–240
7. ^ a b Chow, Ven Te (1959), Open-channel hydraulics, McGraw-Hill, OCLC 4010975, §18-1 & §18-2.
8. ^ a b Cunge, J. A., F. M. Holly Jr. and A. Verwey (1980), Practical aspects of computational river hydraulics, Pitman Publishing, ISBN 0 273 08442 9, §§2.1 & 2.2
9. ^ a b c Whitham, G. B. (1974) Linear and Nonlinear Waves, §§5.2 & 13.10, Wiley, ISBN 0-471-94090-9
10. ^ Lighthill, J. (2005), Waves in fluids, Cambridge University Press, ISBN 978-0-521-01045-0, §§2.8–2.14
11. ^ Meyer, R. E. (1960), Theory of characteristics of inviscid gas dynamics. In: Fluid Dynamics/Strömungsmechanik, Encyclopedia of Physics IX, Eds. S. Flügge & C. Truesdell ,Springer, Berlin, ISBN 978-3-642-45946-7, pp. 225–282
12. ^ a b Didenkulova, I.; Pelinovsky, E. (2011). "Rogue waves in nonlinear hyperbolic systems (shallow-water framework)". Nonlinearity. 24 (3): R1–R18. doi:10.1088/0951-7715/24/3/R01.
13. ^ Harris, M. W.; Nicolsky, D. J.; Pelinovsky, E. N.; Rybkin, A. V. (2015-03-01). "Runup of Nonlinear Long Waves in Trapezoidal Bays: 1-D Analytical Theory and 2-D Numerical Computations". Pure and Applied Geophysics. 172 (3–4): 885–899. Bibcode:2015PApGe.172..885H. doi:10.1007/s00024-014-1016-3. ISSN 0033-4553. S2CID 55004099.
14. ^ Harris, M. W.; Nicolsky, D. J.; Pelinovsky, E. N.; Pender, J. M.; Rybkin, A. V. (2016-05-01). "Run-up of nonlinear long waves in U-shaped bays of finite length: analytical theory and numerical computations". Journal of Ocean Engineering and Marine Energy. 2 (2): 113–127. doi:10.1007/s40722-015-0040-4. ISSN 2198-6444. S2CID 123725815.
15. ^ Garayshin, V. V.; Harris, M. W.; Nicolsky, D. J.; Pelinovsky, E. N.; Rybkin, A. V. (2016-04-10). "An analytical and numerical study of long wave run-up in U-shaped and V-shaped bays". Applied Mathematics and Computation. 279: 187–197. doi:10.1016/j.amc.2016.01.005.
16. ^ Anderson, Dalton; Harris, Matthew; Hartle, Harrison; Nicolsky, Dmitry; Pelinovsky, Efim; Raz, Amir; Rybkin, Alexei (2017-02-02). "Run-Up of Long Waves in Piecewise Sloping U-Shaped Bays". Pure and Applied Geophysics. 174 (8): 3185. Bibcode:2017PApGe.174.3185A. doi:10.1007/s00024-017-1476-3. ISSN 0033-4553. S2CID 132114728.
17. ^ Brunner, G. W. (1995), HEC-RAS River Analysis System. Hydraulic Reference Manual. Version 1.0 Rep., DTIC Document.
18. ^ Searby, D.; Dean, A.; Margetts J. (1998), Christchurch harbour Hydroworks modelling., Proceedings of the WAPUG Autumn meeting, Blackpool, UK.
19. ^ Havnø, K., M. Madsen, J. Dørge, and V. Singh (1995), MIKE 11-a generalized river modelling package, Computer models of watershed hydrology., 733–782.
20. ^ Yeh, G.; Cheng, J.; Lin, J.; Martin, W. (1995), A numerical model simulating water flow and contaminant and sediment transport in watershed systems of 1-D stream-river network, 2-D overland regime, and 3-D subsurface media . Computer models of watershed hydrology, 733–782.
21. ^ DHI (Danish Hydraulic Institute) (2011), MIKE SHE User Manual Volume 2: Reference Guide, ed.
22. ^ Bates, P., T. Fewtrell, M. Trigg, and J. Neal (2008), LISFLOOD-FP user manual and technical note, code release 4.3. 6, University of Bristol.
23. ^ Novak, P., et al., Hydraulic Modelling – An Introduction: Principles, Methods and Applications. 2010: CRC Press.
24. ^ Scharffenberg, W. A., and M. J. Fleming (2006), Hydrologic Modeling System HEC-HMS: User's Manual, US Army Corps of Engineers, Hydrologic Engineering Center.
25. ^ a b Vincent., Fromion (2009). Modeling and control of hydrosystems. Springer. ISBN 9781848826243. OCLC 401159458.
26. ^ "Inclined Planes". www.physicsclassroom.com. Retrieved 2017-05-16.
27. ^ Methods., Haestad (2007). Computer applications in hydraulic engineering : connecting theory to practice. Bentley Institute Press. ISBN 978-0971414167. OCLC 636350249.
28. ^ Dingemans, M.W. (1997), Wave propagation over uneven bottoms, Advanced Series on Ocean Engineering 13, World Scientific, Singapore, pp. 473 & 516, ISBN 978-981-02-0427-3
29. ^ Augier, Pierre; Mohanan, Ashwin Vishnu; Lindborg, Erik (2019-09-17). "Shallow water wave turbulence". Journal of Fluid Mechanics. 874: 1169–1196. doi:10.1017/jfm.2019.375. ISSN 1469-7645. S2CID 198976015.
30. ^ Bühler, Oliver (1998-09-01). "A Shallow-Water Model that Prevents Nonlinear Steepening of Gravity Waves". Journal of the Atmospheric Sciences. 55 (17): 2884–2891. doi:10.1175/1520-0469(1998)055<2884:ASWMTP>2.0.CO;2. ISSN 0022-4928.
31. ^ Lindborg, Erik; Mohanan, Ashwin Vishnu (2017-11-01). "A two-dimensional toy model for geophysical turbulence". Physics of Fluids. 29 (11): 111114. doi:10.1063/1.4985990. ISSN 1070-6631.