Harbor resonance

Resonant waves

Coastal harbors are sensitive to incident waves with frequencies close to the harbor's resonance frequency band. This is especially the case for harbors with vertical walls where incident waves are fully reflected. Resonant wave oscillations in harbors are commonly referred to as seiches. Waves in elongate harbors of length [math]L[/math] and depth [math]h[/math] can resonate if the wave period [math]T[/math] is close to

[math]T=\Large\frac{4L}{(2n+1)c}\normalsize, \; n=0, 1, 2, .. , \qquad (1)[/math]

where [math]c \approx \sqrt{gh}[/math] is the wave celerity, [math]g[/math] the gravitational acceleration and [math]h[/math] the average harbor depth. These wave periods are in general longer than the periods of wind waves and shorter than the periods of tidal components. Significant wave motion in the intermediate period range is usually due to occasional events. Examples include tsunamis caused by seismic events, landslides or atmospheric disturbances. The latter category is the most common and is often referred to as 'meteo tsunamis', see the article Proudman resonance and meteo tsunamis. Fig. 1 illustrates the amplification of a meteo tsunami in the harbor of Rotterdam. The period of the resonant waves is almost one and a half hour, in accordance with the large size of the harbor. In small harbors (marinas), infragravity waves can resonate with periods of less than one minute (see Infragravity waves).

The sensitivity of a harbor to seiches strongly depends on the harbor geometry. Seiche prediction is therefore an important element of harbor design studies. Seiches can impede harbor operations and cause important damage to berthed vessels. The associated currents can even be so strong that mooring lines are broken and that vessels collide with each other and with the quays.

Fig. 1. Amplification of a meteo tsunami in the harbor of Rotterdam. The generation of the meteo tsunami is shown and discussed in the article Proudman resonance and meteo tsunamis. The wave amplitude at the landward harbor end (Rozenburg lock, ROZ) is four times larger than at the seaward boundary (Hook of Holland, HOH). Image from De Jong (2004) with permission.

Seiche amplification factors

The amplification of incident waves at resonance frequencies depends on several factors:

1. Bottom friction. The currents associated with seiches lose momentum by bottom friction. This loss of momentum reduces the wave motion. An approximate formula for wave damping by bottom friction is derived in the appendix for a rectangular harbor basin with uniform depth. The effectiveness of bottom friction for wave damping decreases with increasing depth. This formula also shows that bottom friction alone is generally not sufficient to prevent very strong amplification if the incident wave spectrum is peaked precisely at the resonance frequency of the harbor basin. Frictional damping can be increased artificially, for example by building transverse piers; however, such structures can create currents that are dangerous to navigation.
2. Outward radiation. The reflected wave takes energy away from the basin and thus reduces the wave motion inside. This is illustrated mathematically in the appendix for the simple case of a rectangular harbor basin. The approximate analytical formula shows that outward radiation strongly reduces wave amplification in wide harbors. In narrow harbors (width very small compared to the harbor length), this mechanism is less effective. However, wide harbors are more sensitive to siltation, see Siltation in harbors and fairways. The choice of an optimum harbor design therefore requires careful consideration of these different aspects.
3. Harbor geometry. Rectangular harbors are more sensitive to seiche amplification than harbors with more complex geometry. For example, a deep harbor with shallow side-basins will experience a lower overall amplification due to frictional dissipation and partially destructive interference. Flooding of low harbor quays also reduces the seiche amplitude due to frictional dissipation and a shift of resonance frequency. The example of a harbor with a uniformly sloping floor is discussed in the appendix.

Harbors with a narrow entrance channel

Fig. 2. Sketch of an idealized harbor basin connected to the sea by a narrow channel.

A narrow channel (narrow compared to the harbor basin) connecting a harbor to the sea can greatly modify the harbor resonance frequency. This effect is known as Helmholz resonance. A typical example is Halifax Harbor (Canada), where resonant Helmholz oscillations are observed. Components of the sea level spectrum with a frequency close to the Helmholz resonance frequency are strongly amplified within the harbor basin. Fig. 2 illustrates a harbor with a narrow entrance channel, indicating symbols for depths, widths, lengths, velocity, and water level variation. The Helmholz resonance frequency [math]\sigma_H[/math] is given by

[math]\sigma_H = \omega_0 \, \sqrt{1-\Big(\dfrac{r}{2 \omega_0} \Big)^2}\, , \quad \omega_0 = \sqrt{\dfrac{g b_c h_c}{l_c l_b h_b}} \; . \qquad (2) [/math]

The symbol [math]r[/math] represents the linearized friction coefficient. If the entrance-channel velocity is dominated by the semidiurnal tide with amplitude [math]U[/math], the linearized friction coefficient can be approximated as [math]r = 2 C_D U / h_c[/math], where [math]C_D \sim 1 – 4 \; 10^{-3}[/math] is the dimensionless drag coefficient. The corresponding oscillation period is typically in the range of tenths of minutes to a few hours.

The amplification factor [math]R[/math] associated with Helmholz resonance is

[math]R \equiv \dfrac{a}{a_0} = \dfrac{\omega_0^2}{\sqrt{\big(\omega^2-\omega_0^2)^2 + r^2 \omega^2}} \, , \qquad (3) [/math]

where [math]\omega[/math] is the radial frequency of a spectral sea level component with amplitude [math]a_0[/math] and [math]a[/math] is the corresponding amplitude inside the harbor basin. Spectral sea level components with frequencies on the order of the Helmholz frequency may arise from various processes, including meteorological forcing, infragravity waves, shelf resonance waves or internal waves.

The formulas (1) and (2) are approximations and rely on several hypotheses (see Appendix Helmhoz resonance), notably spatially uniform current velocity in the entrance channel and a resonant wavelength much larger than the harbor basin dimensions [math]l_b[/math] and [math]b_b[/math].

Harbor oscillation modelling

Few harbors have simple geometries that can be modelled with analytical methods. More complex geometries can be simulated well with numerical models. Numerical simulations show that the resonant harbor response strongly depends on the local geometrical layout and bathymetry. Physical scale models can also be used for harbor design studies, but correct simulation of frictional dissipation is not straightforward.

Appendix: Some simple mathematical models

Resonance damping by bottom friction

Fig. 3. Amplification factor [math]a_L/a[/math] of an incident tsunami wave in a harbor of 1000 m length due to bottom friction (linear friction with coefficient [math]F=0.002 \, m/s[/math]).

Here we consider frictional damping of a resonant wave (seiche) in a harbor of length [math]L[/math] and uniform depth [math]h[/math] assuming that friction is linearly dependent on the depth averaged velocity [math]\hat{u}(x,t)[/math]. Other nonlinear terms in the equations of water motion are also ignored, assuming that the wave amplitude is small compared to the water depth. This assumption does not hold for shallow harbors close to resonance. We further assume that the incident wave is monochromatic (angular frequency [math]\omega[/math]) and travels against the outward pointing [math]x[/math]-direction along the longitudinal axis of the harbor. The harbor entrance with seiche amplitude [math]a[/math], is located at [math]x=0[/math], and the harbor head with seiche amplitude [math]a_L[/math], at [math]x=-L[/math]. The time ([math]t[/math]) dependence of the surface elevation [math]\hat{\zeta}(x,t)[/math] and depth averaged velocity [math]\hat{u}(x,t)[/math] is represented by a factor [math]\exp(-i \omega t)[/math]: [math]\hat{\zeta}(x,t)=\Re [\zeta(x) \exp(-i \omega t)], \; \hat{u}(x,t)=\Re [u(x) \exp(-i \omega t)][/math], where the symbol [math]\Re[/math] indicates the real part. The shallow-water equations of motion (mass balance and momentum balance, respectively) then read

[math]-i \omega \zeta +h \Large\frac{du}{dx}\normalsize=0, \quad -i \omega u + g \Large\frac{d \zeta}{dx}\normalsize +F \Large\frac{u}{h}\normalsize =0[/math] ,

where [math]F[/math] is the linear friction coefficient and [math]g=9.8 m^2 \, s^{-1}[/math] the gravitational acceleration. Elimination of [math]u[/math] form these equation gives

[math]\Large\frac{d^2 \zeta}{dx^2}\normalsize + \kappa^2 \zeta = 0, \quad \kappa^2=\Large\frac{\omega^2}{gh}\normalsize (1+\Large\frac{iF}{h \omega}\normalsize) , \quad \zeta (x) = a^+ e^{-i \kappa x} + a^- e^{ i \kappa x}[/math],

[math]\kappa=k-i\mu, \quad k=\Large\frac{\omega}{\sqrt{2gh}}\normalsize\Big[ 1+\big(1+(\Large\frac{F}{h \omega}\normalsize)^2 \big)^{ ½ }\Big]^{ ½ }, \quad \mu =\Large\frac{\omega}{\sqrt{2gh}}\normalsize\Big[ -1+\big(1+(\Large\frac{F}{h \omega}\normalsize)^2 \big)^{ ½ }\Big]^{ ½ }[/math] .

At the end of the harbor ([math]x=-L)[/math] the wave is fully reflected, implying [math]d \zeta /dx=0[/math] (or [math]u=0[/math]). From this condition, expressions for [math]a^{\pm}[/math] can be derived, which give for the surface elevation

[math]\zeta(x)= a_L \Big[ \cosh(\mu (x+L)) \cos(k(x+L)) + i \sinh(\mu (x+L)) \sin(k(x+L)) \Big] .[/math]

The amplification factor [math]R = \Large | \frac{\zeta(x=-L)}{\zeta(x=0)} | \normalsize \equiv \Large\frac{a_L}{a}\normalsize[/math] is given by

[math]\Large\frac{a_L}{a}\normalsize=\Big[ \cosh^2 \mu L \cos^2 kL + \sinh^2 \mu L \sin^2 kL \Big]^{- ½ }[/math].

As an example, the amplification factor of a seiche for a harbor of 1000 m length is shown in Fig. 3 for different depths.

Resonance damping by outward radiation

Fig. 4. Planform of a rectangular harbor on a shelf sea with same uniform depth.

We use here the derivation of Berkhoff (1976), which is similar to the original model of Miles and Munk (1961). The same simplifications and approximations apply as for the previous case, with two exceptions:

• the harbor is considered frictionless ([math]F=0[/math]);
• the reflected wave radiates outward into the unbounded open sea, with the same uniform depth [math]h[/math] as the harbor.

The planform is shown in Fig. 4.

The wave in the harbor [math]\hat{\zeta}_H[/math] is given by

[math]\hat{\zeta}_H(x,t)=\Re [a_L \cos(k(x+L))e^{-i \omega t}][/math].

The incident wave [math]\hat{\zeta}_I[/math] from the sea travels against the [math]x[/math] direction and is given by

[math]\hat{\zeta_{I}}(x,t)= \Re [a e^{-i(kx + \omega t)}][/math].

The wave [math]\hat{\zeta}_R=\zeta_R \, e^{-i \omega t}[/math] that radiates out into the sea has to satisfy the equation

[math]\Large\frac{\partial^2 \hat{\zeta}_R}{\partial t^2}\normalsize - gh \, \Big[\Large\frac{\partial^2 \hat{\zeta}_R}{\partial x^2}\normalsize + \Large\frac{\partial^2 \hat{\zeta}_R}{\partial y^2}\normalsize \Big] =0 \quad[/math] or [math]\quad \omega^2 \zeta_R + gh \, \Big[\Large\frac{\partial^2 \zeta_R}{\partial x^2}\normalsize + \Large\frac{\partial^2 \zeta_R}{\partial y^2}\normalsize \Big] =0[/math]

Fig. 5. Amplification factor [math]a_L/a[/math] of an incident tsunami wave in a frictionless harbor of 1000 m length due to outward radiation of the reflected wave. Adapted from Berkhoff (1976).

Due to the symmetry of the outward radiation, the reflected wave only depends on the distance [math]r[/math] from the harbor entrance. The wave equation in polar coordinates reads

[math]r \Large\frac{\partial^2 \zeta_R}{\partial r^2}\normalsize + \Large\frac{\partial \zeta_R}{\partial r}\normalsize +k^2 r \zeta_R =0 , \qquad k=\Large\frac{\omega}{\sqrt{gh}}\normalsize .[/math]

The solution of this equation satisfying the boundary condition [math]\zeta_R \rightarrow 0[/math] for [math]r \rightarrow \infty[/math] is the Hankel function of the first kind, [math]H_0^{(1)}(kr)[/math]. The asymptotic behaviour for [math]kr \gt \gt 1[/math] of the Hankel function is [math]H_0^{(1)}=\sqrt{\large\frac{2}{ i\pi k r}\normalsize} \, e^{ikr}[/math].

Close to the harbor boundary we have [math]kr \lt \lt 1[/math], assuming that the harbor width is much smaller than the tidal wavelength. Here the Hankel function can be approximated by

[math]H_0^{(1)}(kr) \approx 1+ \large\frac{2i}{\pi}\normalsize \, (\gamma + \ln(kr/2)), \quad \gamma \approx 0.577[/math].

It should be noted that the Hankel function has a singularity at [math]r=0[/math].

The outward radiating wave is a composed by a superposition of waves radiating from different points at the harbor boundary:

[math]\zeta_R (r)= \Large\frac{ a_R }{B}\normalsize \, \int_{-B/2}^{B/2} H_0^{(1)}(kr) dy , [/math]

[math] \zeta_R (x=0) = \Large\frac{ a_R }{B}\normalsize \, \int_{-B/2}^{B/2} H_0^{(1)}(k|y|) dy = 2i a_R D , \quad D= - \Large\frac{i}{2}\normalsize + \Large\frac{1}{\pi}\normalsize (\gamma -1+\ln\Large\frac{kB}{4}\normalsize) . [/math]

Continuity of the surface elevation [math]\zeta[/math] and the derivative [math]d \zeta / dx[/math] at the harbor boundary implies the conditions

[math]\zeta_H=\zeta_I+ \zeta_R \quad[/math] and [math]\quad d \zeta_H /dx= d\zeta_I /dx + d \zeta_R / dr [/math].

The derivative with respect to [math]r[/math] at the harbor entrance ([math]x=0[/math]) is taken at a half circle of radius [math]r=B/2[/math], giving [math]d \zeta_R /dr = 2 i a_R / B .[/math]

Evaluation of the continuity conditions yields the equations

[math]a_L \cos kL=a+2iDa_R \quad[/math] and [math] \quad -ka_L \sin kL=ika+2i \Large\frac{a_R}{B}\normalsize .[/math]

Elimination of [math]a_R[/math] yields the amplification factor [math]R= \Large | \frac{a_L}{a} | \normalsize [/math]:

[math]\Large | \frac{a_L}{a} | \normalsize = \Large | \frac{1-ikBD}{\cos kL + kBD \sin kL} | \normalsize[/math].

As an example, the amplification factor for a harbor of 1000 m length is shown in Fig. 5 for different widths [math]B[/math]. The effectiveness of the radiation mechanism depends primarily on the factor [math]kB=2 \pi B/ \lambda[/math], i.e. the relative width compared to the wavelength [math]\lambda[/math]. Because at resonance the wavelength is proportional to the harbor length [math]L[/math], the wave amplification in the harbor basin depends primarily on the ratio [math]B/L[/math]. The amplification factor increases for decreasing values of [math]B/L[/math].

Sloping harbor floor

The resonance period [math]T[/math] for basins with non-uniform depth is shifted with respect to the resonance period [math]T_0[/math] for basins with uniform depth. As an example, the case of a uniformly sloping harbor floor is considered here, while assuming linear resonance dynamics. Resonance damping by friction and radiation is ignored for simplicity. This assumption is not justified in cases where the harbor is very shallow near the head. Nor can nonlinear effects related to a large amplitude-to-depth ratio be ignored in such cases, which limits the applicability of the results of the linear analysis.

In the linear case, the time ([math]t[/math]) dependence of the surface elevation [math]\hat{\zeta}(x,t)[/math] and depth averaged velocity [math]\hat{u}(x,t)[/math] can be represented by a factor [math]\exp(-i \omega t)[/math]: [math]\hat{\zeta}(x,t)=\Re [\zeta(x) \exp(-i \omega t)], \; \hat{u}(x,t)=\Re [u(x) \exp(-i \omega t)][/math]. The shallow-water equations of motion (mass balance and momentum balance, respectively) then read

[math]-i \omega \zeta + \Large\frac{d (hu)}{dx}\normalsize = 0, \quad -i \omega u + g \Large\frac{d \zeta}{dx}\normalsize = 0 , [/math]

where the depth [math]h[/math] is given by [math]h(x)=h_0+(h_1-h_0)x/L[/math]. Here we use the convention of positive increasing [math]x[/math] from the harbor entrance to the harbor head. The depth [math]h_0[/math] at the harbor entrance [math]x=0[/math] is assumed to be larger than the depth [math]h_1[/math] at the head [math]x=L[/math]. Elimination of the velocity [math]u(x)[/math] from the equations gives

[math]\omega^2 \zeta + g \Large\frac{dh}{dx} \frac{d \zeta}{dx}\normalsize + g h(x) \Large\frac{d^2 \zeta}{dx^2}\normalsize = 0 .[/math]

We introduce the variables [math]x_* = \Large\frac{h_0-h_1}{h_0} \frac{x}{L}\normalsize[/math]. The equation for [math]\zeta[/math] then becomes

[math]\zeta (x_*) \, – \, p^{-2} \Large\frac{d \zeta}{dx_*}\normalsize + p^{-2} (1-x_*) \Large\frac{d^2 \zeta}{dx_*^2}\normalsize =0 , \quad p = \Large\frac{\omega L}{\sqrt{g h_0}}\frac{h_0}{h_0-h_1}\normalsize = \Large\frac{\pi}{2}\frac{T_0}{T}\frac{h_0}{h_0-h_1}\normalsize, \quad T_0=\Large\frac{4 L}{\sqrt{g h_0}}\normalsize.[/math]

Fig. 6. Largest resonance period [math]T[/math] for a basin with uniformly sloping floor from the mouth ([math]h_0[/math]) to the head ([math]h_1[/math]), relative to the resonance period [math]T_0[/math] for a basin with uniform depth [math]h_0[/math]. Results from an analytical solution assuming linear resonance dynamics.

The solution of this equation is

[math]\zeta (x_*) = c_1 J_0 (2p \sqrt{1-x_*}) + c_2 Y_0 (2p \sqrt{1-x_*}) , [/math]

where [math]J_0, \; Y_0[/math] are the Bessel functions of zero order of the first and second kind respectively. The integration constants [math]c_1, \, c_2[/math] are determined from the boundary conditions

[math]\zeta (x_*=0) = a , \quad u(x_*=\Large\frac{h_0-h_1}{h_0}\normalsize) =0 [/math].

The second condition is equivalent to [math]\Large \frac{d \zeta}{dx_*}\normalsize (x_*=\Large\frac{h_0-h_1}{h_0}\normalsize) = p \sqrt{\large\frac{h_0}{h_1}\normalsize} \Big[c_1 J_1 (2p \sqrt{h_1/h_0}) + c_2 Y_1 (2p \sqrt{h_1/h_0}) \Big] = 0 [/math].

Resonance will occur if [math]c_1=\infty[/math] or [math]c_2 = \infty[/math].

From the boundary conditions and the resonance condition it follows that

[math]c_1^{-1} \propto c_2^{-1} \propto J_0(2p) \, Y_1 (2p\sqrt{h_1/h_0}) – Y_0(2p) \, J_1(2p\sqrt{h_1/h_0}) = 0 .[/math]

The periods [math]T[/math] for which resonance occurs can be derived by determining the values of [math]p[/math] satisfying this expression for given values of [math]h_1/h_0[/math]. The corresponding curve [math]T/T_0[/math] is shown in Fig. 6 as a function of [math]h_1/h_0[/math], where [math]T_0[/math] is the resonance period for a basin with uniform depth [math]h_0[/math]. Only the largest resonance period, which usually yields the largest amplification, is shown.

Helmholz resonance

Here we derive Eqs. (2) and (3) for the idealized harbor geometry shown in Fig. 2. The channel and harbor basin are assumed to have negligible spatial and temporal variations in width and depth; hence, these parameters are treated as constants. Because the resonant wavelength is much larger than the characteristic basin dimensions [math]l_b[/math] and [math]b_b[/math], the free surface elevation [math]\eta (t)[/math] may be considered spatially uniform within the basin.

The current velocity [math]u[/math] in the entrance channel is driven by the difference between the free-surface elevation at the offshore boundary and that within the basin. The velocity consists of a tidal component of amplitude [math]U[/math] and a much smaller component [math]u_c[/math] associated with the resonant Helmholz oscillation of the harbor. The pressure-gradient forcing is partly balanced by bottom friction. Since the tidal velocity dominates, the friction term can be linearized, yielding a linear momentum balance for [math]u_c[/math],

[math] \dfrac{d \, u_c}{dt} + \dfrac{g}{l} \Big( \eta(t) - \eta_0 (t) \Big) + r \, u_c = 0 \, , \qquad r = 2 C_D \, U/h_c \; . \qquad (H1)[/math]

In this equation, the velocity [math]u_c[/math] is assumed spatially uniform across the entrance channel. Conservation of mass for the filling and emptying of the harbor basin further requires

[math] b_c \, h_c \, u = b_b \, l_b \dfrac{d \, \eta}{dt} \, . \qquad (H2)[/math]

Eliminating [math]u_c[/math] from the two equations gives

[math]\dfrac{d^2 \eta}{dt^2} + r \, \dfrac{d \, \eta}{dt} + \omega_0^2 \, \eta = \omega_0^2 \, \eta_0 (t) \, , \qquad \omega_0 = \sqrt{\dfrac{g b_c h_c}{l_c l_b h_b}} \, , \qquad (H3)[/math]

which governs the basin free-surface response. For [math]\eta_0=0[/math], Eq. (H1) describes the free unforced oscillation [math]\eta_H[/math] of the harbor basin. Solutions of the form [math]\eta_H (t) \sim \exp(\Sigma t)[/math] yield the characteristic equation

[math]\Sigma^2 + r \, \Sigma + \omega_0^2 =0 \, .[/math]

The imaginary part of [math]\Sigma[/math] defines the Helmholz resonance frequency [math]\sigma_H[/math] given by Eq. (2), while the real part represents frictional damping of the unforced oscillation.

The amplification factor [math]R[/math] for forced Helmholz oscillations follows from solving Eq. (H3) subject to a harmonic sea level forcing at the entrance [math]\eta_0 (t) = a_0 \, \exp(i \, \omega \, t)[/math].

Related articles

Proudman resonance and meteo tsunamis

Siltation in harbors and fairways

References

The main author of this article is Job Dronkers Please note that others may also have edited the contents of this article. Citation: Job Dronkers (2025): Harbor resonance. Available from http://www.coastalwiki.org/wiki/Harbor_resonance [accessed on 23-12-2025] For other articles by this author see Category:Articles by Job Dronkers For an overview of contributions by this author see Special:Contributions/Dronkers J