Abstract
Ocean tides are the oscillatory motions of seawater forced by the gravitational attraction of the Moon and Sun with periods of a half to a day and wavelengths of the semiPacific to Pacific scale. Ocean infragravity (IG) waves are seasurface gravity waves with periods of several minutes and wavelengths of several dozen kilometres. Here we report the first evidence of the resonance between these two ubiquitous phenomena, mutually very different in period and wavelength, in deep oceans. The evidence comes from longterm, largescale observations with arrays of broadband oceanbottom seismometers located at depths of more than 4,000 m in the Pacific Ocean. This observational evidence is substantiated by a theoretical argument that IG waves and the tide can resonantly couple and that such coupling occurs over unexpectedly wide areas of the Pacific Ocean. Through this resonant coupling, some of ocean tidal energy is transferred in deep oceans to IG wave energy.
Introduction
Infragravity (IG) waves are surface waves that are observed in deep^{1} and coastal^{2} oceans. IG waves are strongest near the shoreline^{3}, where they cause harbour oscillations and nearshore processes such as sediment transport^{4}. Disturbances due to IG waves make it difficult to interpret longperiod seismograms at the ocean bottom^{5,6}. Forcing of IG waves is believed to be a major source of Earth's background free oscillations (also known as Earth's hum)^{7,8,9,10,11,12,13,14}. IG waves are mainly generated through nonlinear interactions between highfrequency (period: 20–5 s) wind waves^{15,16}. There are a few reports on the tidal modulation of IG waves in coastal oceans (water depth: 10–30 m)^{17,18,19} and that on the 1,000mdeep shelf^{6}, where the IG wave energy is reduced at low tide. The suggested mechanisms for tidal modulation emphasize the influence of the tide on the generation or decay of IG waves in shallow seas^{19,20}. No tidal modulation has been reported for IG waves in open seas or deep oceans. Here we present the first evidence of the resonance between IG waves and the tide in deep oceans, and show that such resonance can occur over wide areas of the Pacific Ocean.
Results
Modulation of IG waves by ocean tide
We analysed the continuous vertical component records obtained from two broadband oceanbottom seismometer (BBOBS; sensor: Guralp CMG3T) arrays: one (1 February 2003–31 January 2004) with 7 stations (FP array), deployed in French Polynesia^{21} and the other (1 December 2006–30 November 2007) with 11 stations (PS array), deployed in the northern Philippine Sea^{22}. Figure 1 shows the geographical distributions of the stations in these two arrays, which are mostly located at depths of 4,000–5,000 m. Details of the observations are provided in the Methods section. Figure 2a shows two examples of seafloor noise spectra, one obtained from the FP array and the other obtained from the PS array. It has been reported that the spectral peak appearing at ∼10 mHz is a signature of the seafloor disturbance caused by IG waves^{1,5}. This interpretation is supported by Figure 2b, which shows that the depth dependence of the peak frequency in the IG band can be attributed to the hydrodynamic filtering of IG waves. Figure 3 shows the FP array records that are bandpassfiltered between 4 and 20 mHz; in this frequency range, the signal due to the IG waves is dominant. The IG wave trains show temporal variations on a semidiurnal to diurnal scale; however, visual inspection does not reveal any unique periodicity in time coherent through the array. In order to detect any semidiurnal or diurnal periodicity in the IG wave activity coherent across the stations, we divided the 1year record obtained from a station into ∼30day (2.8 × 10^{6} s)long segments with an overlap of ∼10 days (1.0 × 10^{6} s). Each of the 30daylong segments was bandpass filtered between 4 and 20 mHz to extract the IG signals. The negative IG signals were reversed in sign in order to obtain an absolutevalue time series, which was used as a measure of the IG wave activity. The persistency of temporal periodicity among different stations in the same sampling period was examined by normalizing the maximum amplitude of each 30days long record and by calculating a crossspectrum Q_{ij}(f) between stations i and j(≠i). The temporal persistence of the periodicity was examined by constructing crossspectrograms. The crossspectrogram for a station pair i and j is a plot of the crossspectral power Q_{ij}(f) against time. For ease of illustration, we define the stacked crossspectrogram for the ith station as a stack of the crossspectrograms obtained for all pairs of the ith station and the other stations in the same seismic array. Figure 4 shows the stacked crossspectrograms so defined. The frequency ${f}_{{\text{K}}_{1}}$ (period: 23.93 h) of the principal solar tide K_{1}, frequency 2 ${f}_{{\text{M}}_{2}}$ (period: 12.42 h) of the principal lunar tide M_{2}, and its double frequency 2 ${f}_{{\text{M}}_{2}}$ are indicated by arrows along the frequency axis of each stacked crossspectrogram. Note that the intervals between ${f}_{{\text{K}}_{1}}$ and ${f}_{{\text{M}}_{2}}$ and between ${f}_{{\text{M}}_{2}}$ and 2 ${f}_{{\text{M}}_{2}}$ are not equal to each other. The spectral peaks at these three frequencies can be recognized in the spectrograms for almost all time periods and across all the stations. The M_{2} signal is much stronger in the FP spectrograms than in the PS spectrograms, whereas the intensity of the K_{1} signal is almost the same in the FP and PS spectrograms. The second harmonic of the M_{2} signal is considerably weaker than the first harmonic in both the FP and PS spectrograms.
A theory of the resonance between IG waves and the ocean tide
A theory was developed for the coupling of IG waves with the tide in a longwave approximation. Details of this theory are provided in the Methods section. The wave field is assumed to be a random, homogeneous superposition of free IG waves of the form where is the horizontal wavenumber vector and (ref. 23). This assumption is justified by observations made in the deep ocean^{1}. The angular frequency ω is related to k as , where c is the frequencyindependent propagation speed; g, the gravitational acceleration; and H, the water depth. The tidal motion in the local coordinates can be expressed as so that the cophase line of the ocean tide with an angular frequency Ω moves in the direction given by the wavenumber vector and with a speed defined by C≡Ω/K. The fluiddynamic equation of motion including the advection term has a solution of the form showing the tidemodulated IG waves, where the amplification factor R is proportional to In a homogenous random wave field, there is always a wavenumber vector such that with which R undergoes resonant divergence, if
Comparison of the observations and theory
We calculated R for the Pacific Ocean by using the global bathymetry model of ETOPO2^{24} and an ocean tidal model developed by Matsumoto et al.^{25} We set the ω value to the peak frequency in the IG wave band of the seafloor noise at each observational site, as shown by the arrow in Figure 2a. Figure 5a,b show the maps of R for the M_{2} and K_{1} tides, respectively. The area coloured in red is essentially in resonant state, as defined by inequality (1), which may be approximated as c≥C. For a 4,000m ocean depth, c≈200 m s^{−1}, whereas the tidal cophase line at latitude ϑ is expected to move westward with a speed C≈450×cosϑ m s^{−1}, if a laterally uniform ocean covers a laterally uniform Earth. This implies that for a 4,000mdeep uniform ocean, resonance is expected only at high latitudes (ϑ≳65°). Figure 5 demonstrates how different the resonance in the real ocean is from that in the uniform model ocean. In Figure 5, the white area is understood to be in a nearresonance state, where the precise value of R is not calculable according to our firstorder perturbation theory. We can see that unexpectedly wide areas of the Pacific Ocean are in the resonant or nearresonant state. A major part of the FP array is within the resonant area for the M_{2} tide, whereas a major part of the PS array is outside the resonant area; this would be the reason for the M_{2} signal being stronger in the FP array than in the PS array (Fig. 4). On the other hand, a major part of either array is within the resonant area for the K_{1} tide, explaining that the K_{1} signal intensities in the FP and PS arrays are not very different (Fig. 4).
Discussion
Although the abovementioned observations clearly indicate that IG waves in the deep ocean recorded by the BBOBSs are persistently modulated by tidal disturbances, there is a possibility of these waves being apparently modulated by the tiderelated sensitivity change of the instrument. Such a sensitivity change may be caused by tilting of the sensor axis due either to the tidal currents or to the solid Earth tide. Either possibility, however, is unlikely, as will be explained below. Figure 6a,b shows comparisons of the theoretical tides with the tidalband records of the FP array corrected for the instrumental response. In Figure 6a, the comparison is made for the gravity component (corresponding approximately to the vertical displacement) of the theoretical solid Earth tide^{25}. In Figure 6b, the comparison is made for the sea level change (corresponding approximately to the horizontal velocity) of the theoretical ocean tide^{25}. The value attached to each pair of the observed and theoretical traces is a lagtime τ to obtain the best waveform match. In Figure 6a, the observed and theoretical traces are in almost in phase (τ always <0.4 h), indicating that the observed traces are almost π/2 out of phase with the tilt component of the solid tide. In Figure 6b, the observed and theoretical traces are not in phase, where τ increases systematically (from −3.3 to +1.2 h) as we move southwestward through the array (from FP2 to FP8, Fig. 1). Clearly, the vertical records in the tidal band are dominated by the gravity signal due to the solid Earth tide. There is no indication for the vertical records being affected by tilting of the instrument due either to the seafloor tilt or to the tidal current at the BBOBS site. The observed tidal modulation of IG waves should be an actual process occurring in the ocean, rather than an apparent phenomenon caused by the instrumental tilting.
This is further confirmed in Figure 6c, which compares the phase of the observed crossspectrum with and in the same sampling period. Here, and are the crossspectral phases of the tilt component of the theoretical solid Earth tide and the sea surface elevation of the theoretical ocean tide^{25}, respectively. The crosscorrelation function of the observed time series takes only positive values, whereas the crosscorrelation functions of the theoretical tides take both positive and negative values. To account for this difference, a phase in the range 0–2π is reduced to that in the range 0–π. In Figure 6c, the values of and are plotted against for the FP array for the cases where is very large (more than 0.95 times the maximum of over the frequency range shown in Fig. 4). It is apparent that is in better agreement with than with The agreement of with and the absence of ocean tide signals on the records in the tidal band (Fig. 6c) indicate that tidal modulation occurs by coupling between IG waves and the ocean tide in the deep ocean, and not by tideinduced tilting of the sensor axis. If this is the case, the propagation of IG waves may not be perfectly isotropic^{1}, but preferentially parallel to the direction of the cophase lines. This hypothesis can be tested by carrying out longterm, densearray observations of the pressure changes at the sea bottom.
We have shown that free IG waves in the deep ocean are amplified by the resonance with ocean tides and that such resonance can occur over wide areas of the Pacific Ocean. This implies that ocean tides dissipate a certain amount of energy through resonant coupling with IG waves. Our findings suggest the existence of a possible driving force for IG waves in deep oceans and a possible dissipation mechanism of ocean tidal energy in deep oceans^{26,27}.
Methods
A theory of the resonance between IG waves and the ocean tide
Herein, we present a theory of the resonant coupling between IG waves and the ocean tide. In a longwave approximation, the twodimensional equation of motion and the equation for conservation of mass are written as
where is the horizontal velocity vector; ξ, the sea surface elevation; g, the gravitational acceleration; φ, the tidal potential; and H, the water depth^{28}. When H=const and ζ≪H,
To obtain the firstorder solution, we ignore the nonlinear advection term in (2):
Under the assumption that the wave field is random and homogeneous^{23}, the freewave solution can be given as
where
and The freewave (IG wave) propagates in the direction defined by the wavenumber vector with a frequencyindependent speed c. We express the freewaveinduced sea surface elevation as
Substituting this expression in the linearized second equation in (1), we obtain
Without taking into account the detailed form of the tidal potential, we assume that the tidal response can be locally expressed in terms of the horizontal velocity as follows:
so that the cophase line of the tide moves in the direction defined by the wavenumber vector with a speed defined by
The height variation associated with (8) is
with
The firstorder solution is then written as
In a more general case, we assume that the fluid velocity can be expanded in a perturbation series where the firstorder term is given by (12)^{23}. To determine we must make allowance for the nonlinear term. The solution can be obtained by solving the following equation:
When (12) is introduced on the righthand side of (13) and only the interaction terms between free waves and the tide are retained, (13) reduces to
The particular solution of (14) is given by
where
and
Condition for the resonance between IG waves and the ocean tide:
If
there is a wavenumber vector , such that
in a homogeneous random wave field. With such a value, either or becomes infinite in (15), and hence, the IG wave resonates with the tide. The resonance area in the Pacific Ocean, as defined by (17), is shown for the M_{2} tide in Figure 5a and for the K_{1} mode in Figure 5b.
No resonance occurs if
where the sine–sine modulation term dominates the cosine–cosine term in (15). The amplitude of the IG wave becomes maximum when the wavenumber vectors and are in the same direction, so that
where
Thus, in the case of (19), the interaction of an IG wave packet with the tide results in a tidemodulated IG wave packet whose amplitude is R times that of the original wave packet. This amplification factor R may be rewritten as follows, by using (5) and (11):
For the nonresonant area in the Pacific Ocean, as defined by (19), R is plotted for the M_{2} tide in Figure 5a and for the K_{1} mode in Figure 5b. Note that the planewave approximations, as in (8) and (10), may not be valid near the amphidromic point around which the tidal system rotates^{28}. The behaviour near the amphidromic point is beyond the scope of our theory.
Broadband seismic observation at sea bottoms
The BBOBS system has been developed by the Earthquake Research Institute of the University of Tokyo since the 1990s. A BBOBS unit is a selfpopup type, designed to rise from the seafloor after receipt of an acoustic command. The BBOBS with a threecomponent CMG3 T broadband sensor (Guralp Systems) senses ground motions at periods from 0.02 to 360 s with a sampling rate of 100 Hz at 24bit resolution. All of the seismic instrument components, including the sensor, data logger, transponder and batteries, are packed into a 65cm diameter titanium alloy pressure housing, which allows for a maximum operating depth of 6,000 m. The system runs for as long as 500 days to ensure longterm seismic observations. We have practiced more than 50 longterm BBOBS experiments since 1999, including several array observations at the Pacific Ocean seafloor. The locations of all the BBOBS stations are shown in Figure 1.
Additional information
How to cite this article: Sugioka, H. et al. Evidence for infragravity wavetide resonance in deep oceans. Nat. Commun. 1:84 doi: 10.1038/ncomms1083 (2010).
References
 1
Webb, S. C., Zhang, X. & Crawford, W. Infragravity waves in the deep ocean. J. Geophys. Res. 96, 2723–2736 (1991).
 2
Tucker, M. J. Surf beat: sea waves of 1–5 min period. Proc. R. Soc. Lond. A 202, 565–573 (1950).
 3
Elgar, S., Herbers, T. H. C., Okihiro, M., OltmanShay, J. & Guza, R. T. Observations of infragravity waves. J. Geophys. Res. 97, 15573–15577 (1992).
 4
Holman, R. A. & Bowen, A. J. Bars, bumps, and holes: models for the generation of complex beach topography. J. Geophys. Res. 87, 457–468 (1982).
 5
Webb, S. C. Broadband seismology and noise under the ocean. Rev. Geophys. 36, 105–142 (1998).
 6
Dolenc, D., Romanowicz, B., Stakes, D., McGill, P. & Neuhauser, D. Observations of infragravity waves at the Monterey ocean bottom broadband station (MOBB). Geochem. Geophys. Geosyst. 6, Q09002 (2005).
 7
Rhie, J. & Romanowicz, B. Excitation of Earth's continuous free oscillations by atmosphereoceanseafloor coupling. Nature 431, 552–556 (2004).
 8
Rhie, J. & Romanowicz, B. A study of the relation between ocean storms and the Earth's hum. Geochem. Geophys. Geosyst. 7, Q10004 (2006).
 9
Tanimoto, T. The oceanic excitation hypothesis for the continuous oscillations of the Earth. Geophys. J. Int. 160, 276–288 (2005).
 10
Kurrle, D. & WidmerSchnidrig, R. The horizontal hum, of the Earth: a global background of spheroidal and toroidal modes. Geophys. Res. Lett. 35, L06304 (2008).
 11
Webb, S. C. The Earth's 'hum' is driven by ocean waves over the continental shelves. Nature 445, 754–756 (2007).
 12
Bromirski, P. D. & Gerstoft, P. Dominant source regions of the Earth's 'hum' are coastal. Geophys. Res. Lett. 36, L13303 (2009).
 13
Nishida, K., Kawakatsu, H., Fukao, Y. & Obara, K. Background Love and Rayleigh waves simultaneously generated at the Pacific Ocean floors. Geophys. Res. Lett. 35, L16307 (2008).
 14
Fukao, Y., Nishida, K. & Kobayashi, N. Seafloor topography, ocean infragravity waves and background Love and Rayleigh waves. J. Geophys. Res. 115, B04302 (2009).
 15
LonguetHiggins, M. S. & Stewart, R. W. Radiation stress and mass transport in gravity waves, with application to 'surf beats'. J. Fluid Mech. 13, 481–504 (1962).
 16
Herbers, T. H. C., Elgar, S. & Guza, R. T. Generation and propagation of infragravity waves. J. Geophys. Res. 100, 24863–24872 (1995).
 17
Guza, R. T. & Thornton, E. B. Swash oscillations on a natural beach. J. Geophys. Res. 87, 483–491 (1982).
 18
Okihiro, M. & Guza, R. T. Infragravity energy modulation by tides. J. Geophys. Res. 100, 16143–16148 (1995).
 19
Thomson, J., Elgar, S., Raubenheimer, B., Herbers, T. H. C. & Guza, R. T. Tidal modulation of infragravity waves via nonlinear energy losses in the surfzone. Geophys. Res. Lett. 33, L05601 (2006).
 20
Dolenc, D., Romanowicz, B., McGill, P. & Wilcock, W. Observations of infragravity waves at the oceanbottom broadband seismic stations Endeavour (KEBB) and Explorer (KXBB). Geochem. Geophys. Geosyst. 9, Q05007 (2008).
 21
Suetsugu, D. et al. Probing south Pacific mantle plumes with ocean bottom seismographs. EOS Trans. Am. Geophys. Union 86, 429–435 (2005).
 22
Shiobara, H., Baba, K. & Utada, H. Ocean bottom array probes stagnant slab beneath the Philippine Sea. EOS Trans. Am. Geophys. Union 90, 70–71 (2009).
 23
Hasselmann, K. A statistical analysis of the generation of microseisms. Rev. Geophys. 1, 177–210 (1963).
 24
Smith, W. H. F. & Sandwell, D. T. Global sea floor topography from satellite altimetry and ship depth soundings. Science 277, 1956–1962 (1997).
 25
Matsumoto, K., Takanezawa, T. & Ooe, M. Ocean tide models developed by assimilating TOPEX/POSEIDON altimeter data into hydrodynamical model: a global model and a regional model around Japan. J. Oceanography 56, 567–581 (2000).
 26
Munk, W. H. & Macdonald, G. J. F. The Rotation of the Earth (Cambridge University Press, 1960).
 27
Munk, W. H. & Wunsch, C. Abyssal recipes II: energetics of tidal and wind mixing. DeepSea Res. 45, 1977–2010 (1998).
 28
Apel, J. R. Principles of Ocean Physics (Academic, 1987).
 29
Peterson, J. Observations and modelling of seismic background noise. USGS OpenFile Report 93–322 (1993).
Acknowledgements
We thank Hajime Shiobara, Earthquake Research Institute, University of Tokyo, and Daisuke Suetsugu, Japan Agency for MarineEarth Technology (JAMSTEC), for organizing the BBOBS observation experiments. We are also thankful to the captains and crew of the research vessels and the Shinkai6500 operation team of JAMSTEC for their valuable support during the cruises. This study was supported by a GrantinAid for Scientific Research from the Japan Society for the Promotion of Science (19740282).
Author information
Affiliations
Contributions
H.S. carried out observations and analysed the obtained data; Y.F. proposed the theory; and T.K. developed the observation system.
Corresponding author
Correspondence to Hiroko Sugioka.
Ethics declarations
Competing interests
The authors declare no competing financial interests.
Rights and permissions
About this article
Cite this article
Sugioka, H., Fukao, Y. & Kanazawa, T. Evidence for infragravity wavetide resonance in deep oceans. Nat Commun 1, 84 (2010). https://doi.org/10.1038/ncomms1083
Received:
Accepted:
Published:
Further reading

Location of Seismic “Hum” Sources Following Storms in the North Pacific Ocean
Geochemistry, Geophysics, Geosystems (2019)

Infragravity Wave Generation by Wind Gusts
Geophysical Research Letters (2019)

Excitation Location and Seasonal Variation of Transoceanic Infragravity Waves Observed at an Absolute Pressure Gauge Array
Journal of Geophysical Research: Oceans (2018)

Ambient seismic wave field
Proceedings of the Japan Academy, Series B (2017)

Source characteristics of ocean infragravity waves in the Philippine Sea: analysis of 3year continuous network records of seafloor motion and pressure
Earth, Planets and Space (2014)
Comments
By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.