Proudman resonance and meteo tsunamis
Definition of Meteo tsunamis:
Meteo tsumanis are long ocean surface oscillations generated by intense atmospheric disturbances travelling over the open sea.
This is the common definition for Meteo tsunamis, other definitions can be discussed in the article

The frequency band of meteo tsunamis waves corresponds to that of seismically generated tsunamis, which explains their naming. They are sometimes also called nonseismic sealevel oscillations at tsunami timescales (NSLOTTs). They are recorded on most continental shelves globally, where strong secondary amplification can occur due to topographic resonance effects^{[1]} (see Harbor resonance). Regionally, meteo tsunamis are known by different local names: rissaga (Spain’s Balearic Islands and New Zealand), abiki (Japan’s Nagasaki Bay), sciga (Adriatic), milghuba (Malta), marrobbio (Sicily), seebär (Baltic Sea)^{[2]}. Amplification by Proudman resonance occurs when an atmospheric disturbance travels over large distances (hundred kilometers or more) at approximately the same speed as the propagation celerity of long ocean waves^{[3]}^{[4]}^{[5]}. Although meteo tsunamis are only a minor component of the overall sealevel oscillations, they can cause sealevel extremes and flooding, especially when combined with higher tides and storm surges, on top of the increased mean sea levels^{[6]}. In some cases they are also capable of generating strong rip currents^{[7]}.
Contents
Generation of meteo tsunamis
Local atmospheric pressure disturbances above open water generate wave motions at the water surface. Meteo tsunamis are often associated with midtroposphere jet streams and instability of the troposphere in the zone around 500 hPa^{[6]}. The periods of meteoinduced water waves are typically in the range of a few minutes to a few hours, i.e. intermediate between wind waves and tidal waves. The amplitude of these waves is generally small (typically in the cm range) compared to wind waves and tidal waves. However, in some cases they can be strongly amplified. This occurs when the pressure perturbation advances at a speed comparable to the propagation speed (celerity) of the surface waves in the water body. This amplification is known as Proudman resonance, after the scientist who first demonstrated this phenomenon^{[3]}. When meteoinduced water waves are strongly amplified they are often called meteo tsunamis, because their period is in the same range where tsunamis caused by other phenomena occur, such as submarine earthquakes and landslides – see the article Tsunami. Various atmospheric processes can generate meteo tsunamis, for example frontal passages, gales, squalls, storms, orographic influence and tornados. Examples of meteo tsunamis are shown in Figs. 1 and 2.
Proudman resonance
Whether the propagation speed [math]V[/math] of an atmospheric pressure disturbance is comparable to the celerity [math]c[/math] of long surface waves depends on the depth of the water body, which can be approximated by [math]c=\sqrt{gh}[/math], where [math]h[/math] is the local water depth and [math]g \approx 9.8 \, m^2 s^{1}[/math] the gravitational acceleration. In deep ocean water the wave propagation celerity is always much larger (typically in the order of 200 m/s) than the speed of atmospheric pressure disturbances (typically in the order of 1050 m/s). However, on the continental shelf (depths between 50 and 500 m), the speed can be comparable and Proudman resonance can occur. The mathematical derivation by Proudman is presented in the appendix.
Harbor seiches
Proudman resonance can amplify the initial meteoinduced water wave by a factor 510 if the propagation speeds of the atmospheric disturbance and the water wave are on average about the same^{[10]}. Even in this case the amplitude of the meteo tsunami will seldom exceed a few decimeters. Waves of this amplitude generally do not cause great harm. However, further amplification can occur if the wave period is close to the resonance period of coastal topographic features, such as semienclosed bays and basins. Many harbors resonate at wave periods in the same range as the periods of meteo tsunamis, on the order of one minute period for small harbors and on the order of one hour for large harbors (the basic resonance period of an elongate harbor of length [math]L[/math] and depth [math]h[/math] is given by [math]4L/\sqrt{gh}[/math]). If the harbor resonance period and the wave period match, a further wave amplification with a factor 510 is possible^{[11]}. Resonant harbor waves are called seiches. For a more detailed discussion of this phenomenon, the reader is referred to the article Harbor resonance. Harbor seiches can cause considerable damage to berthed vessels and harbor infrastructure (Fig. 3).
Not all meteo tsunamis are amplified by Proudman resonance. Strong typhoons can generate long surface oscillations of considerable amplitude when amplified by topographic resonance effects^{[12]}.
Appendix: A simple mathematical model of Proudman resonance
The simple model, first described by Proudman^{[3]}, considers the following idealised situation:
 Continental shelf of uniform depth [math]h[/math],
 The influence of friction, tide and earth's rotation are neglected.
The pressure disturbance is assumed uniform in [math]y[/math]direction and moves without deformation in [math]x[/math]direction with velocity [math]V[/math]. The disturbance is then given by [math]p=g \rho f(xVt)[/math], where [math]\rho[/math] is water density and [math]g[/math] the gravitational acceleration. The shallowwater equations of motion read
[math]\Large\frac{\partial u}{\partial t}\normalsize + g \Large\frac{\partial \zeta}{\partial x}\normalsize =  \Large\frac{1}{\rho}\frac{\partial p}{\partial x}\normalsize , \quad h\Large\frac{\partial u}{\partial x}\normalsize + \Large\frac{\partial \zeta}{\partial t}\normalsize = 0[/math].
Symbols are: [math]\zeta=[/math] sea surface elevation, [math]u=[/math] current velocity and [math]t=[/math] time.
Elimination of [math]u[/math] gives the equation [math]\Large\frac{\partial^2 \zeta}{\partial t^2}\normalsize gh\Large\frac{\partial^2 \zeta}{\partial x^2}\normalsize = gh\Large\frac{\partial^2 }{\partial x^2} \normalsize f(xVt)[/math].
The general solution reads
[math]\zeta(x,t)=\zeta^{(1)}(xct)+ \zeta^{(2)}(x+ct)+ \zeta^{(3)}(xVt), \qquad \zeta^{(3)}=\Large\frac{f}{1(V/c)^2}\normalsize , \quad c=\sqrt{gh}[/math].
The functions [math]\zeta^{(1)}[/math] and [math]\zeta^{(2)}[/math] are determined by the initial conditions [math]\zeta=0, u=0[/math] at [math]t=0[/math]. Evaluation of these conditions yields
[math]\zeta(x,t)=\Large\frac{1}{1(V/c)^2}\normalsize \Big[ f(xVt)  \Large\frac{1}{2}\normalsize (1+\Large\frac{V}{c})\normalsize f(xct)  \Large\frac{1}{2}\normalsize (1\Large\frac{V}{c})\normalsize f(x+ct) \Big] [/math].
If the propagation speed of the disturbance is close to the wave celerity, [math]V =c+\Delta c[/math], and if [math] t \Delta c[/math] is much smaller than the spatial scale [math]L[/math] of the pressure field, then the expression of [math]\zeta[/math] can be approximated by
[math]\rho g \zeta(x,t) \approx \large\frac{1}{4}\normalsize \Big( p(x+Vt)p(xVt) \Big)  \Large\frac{Vt}{2}\frac{\partial}{\partial x} \normalsize p(xVt), \qquad x \le Vt[/math].
In this case we have Proudman resonance: the amplitude of the meteoinduced propagating wave increases linearly with time. The amplitude also depends linearly on the atmospheric pressure gradient, i.e. the steepness of the atmospheric disturbance that travels with speed [math]V[/math] approximately equal to the water wave celerity [math]dx/dt=c[/math]. It can be shown that these results remain qualitatively valid even if the conditions of this simple model are not strictly met^{[5]}.
Related articles
References
 ↑ Vilibic, I. and Sepic, J., 2009. Destructive meteotsunamis along the eastern Adriatic coast: overview. Phys. Chem. Earth 34: 904–917
 ↑ Pattiaratchi, C. and Wijeratne, E.M.S. 2014. Observations of meteorological tsunamis along the southwest Australian coast. Nat. Hazards 74: 281–303
 ↑ ^{3.0} ^{3.1} ^{3.2} Proudman, J. 1929. The effects on the sea of changes in atmospheric pressure. Geophys J. Int. 2: 197–209 Cite error: Invalid
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tag; name "P" defined multiple times with different content  ↑ Williams, D.A., Schultz, D.M., Horsburgh, K.J. and Hughes, C.W. 2021. An 8yr meteotsunami climatology across Northwest Europe: 2010–17. J. Phys. Oceanogr. 51: 1145–1161
 ↑ ^{5.0} ^{5.1} Williams, D.A., Horsburgh, K.J., Schultz, D.M. and Hughes, C.W., 2021. Proudman resonance with tides, bathymetry and variable atmospheric forcings. Nat. Hazards 106: 1169–1194
 ↑ ^{6.0} ^{6.1} Zemunik, P., Denamiel, C., Sepic, J. and Vilibic, I. 2022. Highfrequency sealevel analysis: Global distributions. Global and Planetary Change 210, 103775
 ↑ Linares, A., Wu, C.H., Bechle, A.J., Anderson, E.J. and Kristovich, D.A.R. 2019. Unexpected rip currents induced by a meteotsunami. Nature Sci. Rep. 9: 2105
 ↑ Villalonga, J., Monserrat, S., Gomis, D. and Jordà, G. 2024. Observational characterization of atmospheric disturbances generating meteotsunamis in the Balearic Islands. Journal of Geophysical Research: Oceans 129, e2024JC020910
 ↑ De Jong, M.P.C. 2004. Origin and prediction of seiches in Rotterdam harbour basins. PhD thesis Delft University.
 ↑ ^{10.0} ^{10.1} Monserrat, S., Vilibic, I. and Rabinovich, A.B. 2006. Meteotsunamis: atmospherically induced destructive ocean waves in the tsunami frequency band. Natural Hazards and Earth System Sciences 6: 1035–1051
 ↑ Rabinovich, A.B. 2009. Seiches and harbor oscillations. In: Handbook of Coastal and Ocean Engineering (Ed. Y.C. Kim). World Scientific Publ., Singapore
 ↑ Heidarzadeh, M. and Rabinovich, A.B. 2021. Combined hazard of typhoongenerated meteorological tsunamis and storm surges along the coast of Japan. Nat. Hazards 106: 1639–1672
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