Difference between revisions of "Bathymetry from remote sensing wave propagation"

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==Surface topographic patterns==
 
==Surface topographic patterns==
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Water motion produces undulation patterns at the water surface that contain information about the seafloor bathymetry. This offers the possibility to determine the bathymetry through observation of specific features of the water surface topography. Over the past fifty years, various techniques have been developed that provide information about patterns at the water surface. These techniques use remote sensing and require much less measurement effort than traditional measurements carried out with ships. On the other hand, unlike direct ship-based measurements of water depth, remote sensing data provides indirect information that can only be interpreted using advanced analysis techniques. This article discusses some of the processes that determine the relationship between bathymetry and surface undulation patterns. The focus is on the nearshore zone and surface patterns produced by propagating waves.
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Water motion produces undulation patterns at the water surface that contain information about the seafloor bathymetry. This offers the possibility to determine the bathymetry through observation of specific features of the water surface topography. Over the past fifty years, various techniques have been developed that provide information about patterns at the water surface. These techniques use remote sensing and require much less measurement effort than traditional measurements carried out with ships. On the other hand, unlike direct ship-based measurements of water depth, remote sensing data provides indirect information that can only be interpreted using advanced analysis techniques. In addition, bathymetry determination based on wave remote sensing is inherently limited by the wavelengths and time in which propagating waves respond to a spatially varying bottom<ref>Almar, R., Bergsma, E. W., Thoumyre, G., Baba, M. W., Cesbron, G., Daly, C., Garlan, T. and Lifermann, A. 2021. Global satellite-based coastal bathymetry from waves. Remote Sensing 13, 4628</ref>. The most accurate results are obtained when substantial waves form a regular surface pattern, as in the case of large swell waves.
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This article discusses some of the processes that determine the relationship between bathymetry and surface undulation patterns. The focus is on the nearshore zone and surface patterns produced by propagating waves.
  
 
Several remote sensing techniques can be used to determine wave patterns at the water surface:
 
Several remote sensing techniques can be used to determine wave patterns at the water surface:
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* Satellite optical imagery<ref> Almar, R., Bergsma, E.W., Thoumyre, G., Baba, M.W., Cesbron, G., Daly, C., Garlan, T. and Lifermann, A. 2021. Global satellite-based coastal bathymetry from waves. Remote Sensing 13, 4628</ref>, see [[Satellite-derived nearshore bathymetry]]
 
* Satellite optical imagery<ref> Almar, R., Bergsma, E.W., Thoumyre, G., Baba, M.W., Cesbron, G., Daly, C., Garlan, T. and Lifermann, A. 2021. Global satellite-based coastal bathymetry from waves. Remote Sensing 13, 4628</ref>, see [[Satellite-derived nearshore bathymetry]]
  
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In this article we will not discuss the retrieval of surface wave patterns from remote sensing images; information can be found in the articles cited above. Without giving details of how this is done, we will assume that wavelength, wave period and wave height can be determined from the remote sensing images in every point of the considered nearshore area.
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In this article we will not discuss the retrieval of surface wave patterns from remote sensing images; information can be found in the articles cited above. In the following we will assume that wavelength, wave period and wave height can be determined from the remote sensing images in every point of the considered nearshore area.
  
  
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The wave dispersion relation is the key to determining bathymetry from the wavelength <math>\lambda</math>, the wave period <math>T = 2 \pi / \omega</math> and the wave height <math>H</math>. According to linear wave theory, the wave dispersion relation can be written as  
 
The wave dispersion relation is the key to determining bathymetry from the wavelength <math>\lambda</math>, the wave period <math>T = 2 \pi / \omega</math> and the wave height <math>H</math>. According to linear wave theory, the wave dispersion relation can be written as  
  
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<math>c = \Large\frac{gT}{2 \pi }\normalsize \, \tanh kh , \qquad (1)</math>
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<math>c = u + \Large\frac{gT}{2 \pi }\normalsize \, \tanh kh , \qquad (1)</math>
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where <math>c  = \lambda / T = \omega / k</math> is the wave celerity, <math>k = 2 \pi / \lambda</math> is the wave number (the length of the wave number vector <math>\vec{k}</math>), <math>\omega</math> is the radial wave frequency, <math>g \approx 9.8  \; ms^{-2}</math> is the gravitational acceleration, <math>h</math> is the still water depth and <math>u</math> is the surface current velocity in the wave propagation direction. In the following we assume that the surface current velocity is nil or very small, <math>u << c</math>. If this condition is not satisfied but the surface current velocity is known, it can be subtracted from the measured wave celerity <math>c</math>. In the converse case where the bathymetry is known and the surface current velocity is substantial but unknown, the component <math>u</math> of the surface current velocity in the direction of the wave propagation velocity can be determined by observation of the wave propagation velocity <math>c</math> <ref>Streßer, M., Carrasco, R. and Horstmann, J. 2017. Video-based estimation of surface currents using a low-cost quadcopter. Geosci. Rem. Sens. Lett. IEEE 14: 2027–2031</ref><ref>Fairley, I., King, N., McIlvenny, J., Lewis, M., Neill, S., Williamson, B.J., Masters, I. and Reeve, D.E. 2024. Intercomparison of surface velocimetry techniques for drone-based marine current characterization. Estuarine, Coastal and Shelf Science 299, 108682</ref>.
  
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where <math>c  = \lambda / T = \omega / k</math> is the wave celerity, <math>k = 2 \pi / \lambda</math> is the wave number (the length of the wave number vector <math>\vec{k}</math>), <math>\omega</math> is the radial wave frequency and <math>h</math> is the still water depth. The local water depth <math>h</math> can be found by inversion of this formula:
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The local water depth <math>h</math> can be found by inversion of formula (1):
  
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<math>h = \Large\frac{1}{k }\normalsize \, \tanh^{-1} \Big(  \Large\frac{2 \pi c}{g T}\normalsize  \Big), \qquad (2)</math>
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<math>h = \Large\frac{1}{k }\normalsize \, \tanh^{-1} \Big(  \Large\frac{2 \pi c}{g T}\normalsize  \Big) . \qquad (2)</math>
  
 
In shallow water, <math> kh << 1</math>, the relationship (1) between water depth and wave celerity becomes <math>c^2 \approx gh</math>. Knowledge of the wave celerity is sufficient to determine the water depth. In deep water, <math>k h  > 1</math>, and <math>\tanh kh \approx 1</math>. According to Eq. (1), the wave celerity in deep water does not depend on the depth, meaning that the depth cannot be determined from inversion of the dispersion relation.
 
In shallow water, <math> kh << 1</math>, the relationship (1) between water depth and wave celerity becomes <math>c^2 \approx gh</math>. Knowledge of the wave celerity is sufficient to determine the water depth. In deep water, <math>k h  > 1</math>, and <math>\tanh kh \approx 1</math>. According to Eq. (1), the wave celerity in deep water does not depend on the depth, meaning that the depth cannot be determined from inversion of the dispersion relation.
  
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Another restriction on the use of Eq. (1) are the assumptions underlying linear wave theory. These assumptions are: (i) irrotational wave flow, (ii) <math>H/h <<1</math> and (iii) <math>H / \lambda <<1</math>. However, these assumptions are not satisfied in the nearshore zone where waves become skewed and asymmetric.
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Other restrictions on the use of Eq. (1) are the assumptions underlying linear wave theory. These assumptions are: (i) irrotational wave flow, (ii) the wave amplitude <math>H</math> is much smaller than the water depth (<math>H/h <<1</math>) and (iii) much smaller than the wavelength (<math>H / \lambda <<1</math>). However, these assumptions are not satisfied in the nearshore zone where waves become skewed and asymmetric and eventually break.
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If weak nonlinearity is assumed in the shoaling zone (prior to wave breaking) nonlinear Stokes theory can be applied if the Ursell number <math>U_r = kH / (kh)^3</math> is small. In this case the dispersion relation can be approximated by<ref>Whitham, G.B. 1974. Linear ands nonlinear waves. Wiley-Interscience</ref>
 
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<math>c = \Large\frac{gT}{2 \pi }\normalsize \, \sigma  \Big( 1 + \Large\frac{9 - 10 \sigma^2+9 \sigma^4}{32 \sigma^4}\normalsize  (kH)^2 \Big) + O[(kH)^4]  , \qquad 
 
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\sigma = \tanh kh  .\qquad (3)</math>
 
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From this formula <math>\sigma</math> and <math>h</math> can be determined by a numerical inversion procedure.
 
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Field observations of wave height and wave celerity show that the shallow water linear dispersion relation underestimates the wave speed at wave breaking and inside the surf zone. Measured celerity values can be 20% higher than predicted by the linear dispersion relation<ref name=TG/> or even more<ref>Suhayda, I.N. and Pettigrew, N.R. 1977. Observations of wave height and wave celerity in the surf zone. J. Geophys. Res. 82: 1419-1424</ref>. Weak nonlinearity cannot be assumed in the zone where waves are breaking. If the wave after breaking is surfing onshore like a bore, the bore formula for the celerity can be applied (see [[Tidal bore dynamics]], Eq. (1) ),
 
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<math>c = \sqrt{gh} \, \sqrt{(1+\large\frac{H}{h}\normalsize)(1+\large\frac{H}{2h}\normalsize)} . \qquad (4)</math> 
 
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An alternative approach is applying cnoidal wave theory. This gives<ref name=TG>Thornton, E.B. and Guza, R.T. 1982. Energy saturation and phase speeds measured on a natural beach. J. Geophys. Res. 87, 9499</ref>
 
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<math>c \approx \sqrt{g h} \, \sqrt{1 + \alpha \large\frac{H}{h}\normalsize } , \qquad (5)</math>
 
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where <math>\alpha</math> is a function of the Ursell number with value close to 1. Empirical evidence<ref>Holland, T.K. 2001. Application of the linear dispersion relation with respect to depth inversion and remotely sensed imagery. IEEE Trans. on Geos. and Rem. Sens. 39: 2060-2071</ref> suggests <math>c \approx \sqrt{g h} \, \sqrt{1 + 0.45 \large\frac{H_s}{h}\normalsize } </math>, where <math>H_s</math> is the significant wave height. 
 
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A physics-based approach uses a modified dispersion relation according to the Boussinesq theory that describes the propagation of weakly nonlinear and weakly dispersive waves for Ursell numbers of order unity (<math>O[H/h] \sim O[(kh)^2] <<1</math>). In this theory, nonlinear interactions between resonant triads of frequencies (<math>\omega, \pm \omega', \omega \mp \omega'</math>) lead to the growth of forced high-frequency components that modify the wave shape in shallow water. The resulting dispersion relation to order <math>(kh)^2</math> is<ref>Herbers, T.H.C., Elgar, S., Sarap, N.A. and Guza, R.T. 2002. Nonlinear dispersion of surface gravity waves in shallow water. Journal of Physical Oceanography 32: 1181–1193</ref><ref name=M22>Martins, K., Bonneton, P., de Viron, O., Turner, I.L.,  Harley, M.D. and Splinter, K. 2022. New Perspectives for Nonlinear Depth-Inversion of the Nearshore Using Boussinesq Theory. Geophysical Research Letters 50, e2022GL100498</ref>
 
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<math>c(\omega) = \Large\frac{\omega}{k(\omega)}\normalsize = \sqrt{gh} \Big[ 1 + \Large\frac{h \omega^2}{3g} + \frac{h^2 \omega^4}{36g^2} - \frac{1}{h}\normalsize \gamma_{am} \Big]^{-1/2} , \qquad \gamma_{am} = \Large\frac{3}{2 | \hat{\eta}(\omega)|^2}\normalsize \, \int_{-\infty}^{\infty} \Re \big( \hat{\eta}(\omega')  \hat{\eta}(\omega - \omega') \hat{\eta}^*(\omega) \big) d \omega' , \qquad (6)</math>
 
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where <math>\hat{\eta}(\omega) = \hat{\eta}(k, \omega)</math> is the Fourier transform of the surface elevation <math>\eta (x, t) = \int \int \hat{\eta}(k, \omega) \exp(i(kx-\omega t)) dk d\omega</math>. Application of this dispersion relation requires datasets of the free surface elevation with high space and time resolution from which <math>\hat{\eta}(\omega)</math> can be determined. Lidars currently offer the most robust and practical solution for collecting such highly-resolved surface elevation data in the field. The depth <math>h</math> can be determined from Eq. (6) by a least-squares fit to values of <math>c(\omega)</math> around the peak wave frequency<ref name=M22/>. Using this theory, reasonable agreement was found (within 10%) in laboratory experiments between the real depth profiles in the shoaling and surf zones and depth profiles derived from the interpretation of water surface patterns using the dispersion relation Eq. (6) <ref name=M22/>.  
 
  
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Although equation (2) generally provides a reasonable approximation, it may be necessary to use more accurate formulas that take into account the nonlinearity of wave propagation in shallow water. Dispersion relations for nonlinear wave propagation are given in the article [[Nonlinear wave dispersion relations]]. Application of these formulas require knowledge of the wave height <math>H</math> or even the whole wave field. The water depth <math>h</math> can be determined by numerical inversion of the dispersion relations. 
  
  
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==Symbols==
 
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{| class="wikitable"
 
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|-
 
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! Variable !! Description !! Variable !! Description !! Variable !! Description
 
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|-
 
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| <math>c = \omega / k</math> || wave celerity || <math>H</math> || wave height ||<math>x</math>||  cross-shore coordinate
 
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|-
 
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| <math>g</math> || gravitational acceleration || <math>t</math>|| time ||<math>\eta(x,t)</math>|| wave surface elevation
 
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|-
 
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| <math>k = 2 \pi / \lambda</math>|| wave number || <math>T</math>|| wave period ||<math>\lambda</math>|| wavelength
 
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|-
 
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| <math>h = h(x)</math>||  local still water depth  || <math>U_r = kH / (kh)^3</math>|| Ursell number ||<math>\omega</math>|| radial wave frequency
 
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|}
 
  
 
==Related articles==
 
==Related articles==
 +
:[[Nonlinear wave dispersion relations]]
 
:[[Use of X-band and HF radar in marine hydrography]]
 
:[[Use of X-band and HF radar in marine hydrography]]
 
:[[Satellite-derived nearshore bathymetry]]
 
:[[Satellite-derived nearshore bathymetry]]

Latest revision as of 15:47, 1 September 2024


Surface topographic patterns

Water motion produces undulation patterns at the water surface that contain information about the seafloor bathymetry. This offers the possibility to determine the bathymetry through observation of specific features of the water surface topography. Over the past fifty years, various techniques have been developed that provide information about patterns at the water surface. These techniques use remote sensing and require much less measurement effort than traditional measurements carried out with ships. On the other hand, unlike direct ship-based measurements of water depth, remote sensing data provides indirect information that can only be interpreted using advanced analysis techniques. In addition, bathymetry determination based on wave remote sensing is inherently limited by the wavelengths and time in which propagating waves respond to a spatially varying bottom[1]. The most accurate results are obtained when substantial waves form a regular surface pattern, as in the case of large swell waves.

This article discusses some of the processes that determine the relationship between bathymetry and surface undulation patterns. The focus is on the nearshore zone and surface patterns produced by propagating waves.

Several remote sensing techniques can be used to determine wave patterns at the water surface:

In this article we will not discuss the retrieval of surface wave patterns from remote sensing images; information can be found in the articles cited above. In the following we will assume that wavelength, wave period and wave height can be determined from the remote sensing images in every point of the considered nearshore area.


Depth inversion algorithms

The wave dispersion relation is the key to determining bathymetry from the wavelength [math]\lambda[/math], the wave period [math]T = 2 \pi / \omega[/math] and the wave height [math]H[/math]. According to linear wave theory, the wave dispersion relation can be written as

[math]c = u + \Large\frac{gT}{2 \pi }\normalsize \, \tanh kh , \qquad (1)[/math]

where [math]c = \lambda / T = \omega / k[/math] is the wave celerity, [math]k = 2 \pi / \lambda[/math] is the wave number (the length of the wave number vector [math]\vec{k}[/math]), [math]\omega[/math] is the radial wave frequency, [math]g \approx 9.8 \; ms^{-2}[/math] is the gravitational acceleration, [math]h[/math] is the still water depth and [math]u[/math] is the surface current velocity in the wave propagation direction. In the following we assume that the surface current velocity is nil or very small, [math]u \lt \lt c[/math]. If this condition is not satisfied but the surface current velocity is known, it can be subtracted from the measured wave celerity [math]c[/math]. In the converse case where the bathymetry is known and the surface current velocity is substantial but unknown, the component [math]u[/math] of the surface current velocity in the direction of the wave propagation velocity can be determined by observation of the wave propagation velocity [math]c[/math] [11][12].

The local water depth [math]h[/math] can be found by inversion of formula (1):

[math]h = \Large\frac{1}{k }\normalsize \, \tanh^{-1} \Big( \Large\frac{2 \pi c}{g T}\normalsize \Big) . \qquad (2)[/math]

In shallow water, [math] kh \lt \lt 1[/math], the relationship (1) between water depth and wave celerity becomes [math]c^2 \approx gh[/math]. Knowledge of the wave celerity is sufficient to determine the water depth. In deep water, [math]k h \gt 1[/math], and [math]\tanh kh \approx 1[/math]. According to Eq. (1), the wave celerity in deep water does not depend on the depth, meaning that the depth cannot be determined from inversion of the dispersion relation.

Other restrictions on the use of Eq. (1) are the assumptions underlying linear wave theory. These assumptions are: (i) irrotational wave flow, (ii) the wave amplitude [math]H[/math] is much smaller than the water depth ([math]H/h \lt \lt 1[/math]) and (iii) much smaller than the wavelength ([math]H / \lambda \lt \lt 1[/math]). However, these assumptions are not satisfied in the nearshore zone where waves become skewed and asymmetric and eventually break.

Although equation (2) generally provides a reasonable approximation, it may be necessary to use more accurate formulas that take into account the nonlinearity of wave propagation in shallow water. Dispersion relations for nonlinear wave propagation are given in the article Nonlinear wave dispersion relations. Application of these formulas require knowledge of the wave height [math]H[/math] or even the whole wave field. The water depth [math]h[/math] can be determined by numerical inversion of the dispersion relations.


Related articles

Nonlinear wave dispersion relations
Use of X-band and HF radar in marine hydrography
Satellite-derived nearshore bathymetry
Bathymetry German Bight from X-band radar
Waves and currents by X-band radar
Statistical description of wave parameters


References

  1. ↑ Almar, R., Bergsma, E. W., Thoumyre, G., Baba, M. W., Cesbron, G., Daly, C., Garlan, T. and Lifermann, A. 2021. Global satellite-based coastal bathymetry from waves. Remote Sensing 13, 4628
  2. ↑ Bergsma, E.W.J., Almar, R., de Almeida, L. P.M. and Sall, M. 2019. On the operational use of UAVs for video-derived bathymetry. Coastal Engineering 152, 103527
  3. ↑ Lange A.M.Z., Fiedler, J.W., Merrifield, M.A. and Guza, R.T. 2023. UAV video-based estimates of nearshore bathymetry. Coastal Engineering 185, 104375
  4. ↑ Stockdon, H.F. and Holman, R.A. 2000. Estimation of wave phase speed and nearshore bathymetry from video imagery. Journal of Geophysical Research 105(C9): 22015–22033
  5. ↑ Aarninkhof, S.G.J., Ruessink, B.G. and Roelvink, J.A. 2005. Nearshore subtidal bathymetry from time-exposure video images. J. Geophys. Res. 110, C06011
  6. ↑ Fiedler, J.W., Kim, L., Grenzeback, R. L., Young, A.P. and Merrifield, M.A. 2021. Enhanced surf zone and wave runup observations with hovering drone-mounted lidar. Journal of Atmospheric and Oceanic Technology 38(11): 1967–1978
  7. ↑ Bell, P. S. 1999. Shallow water bathymetry derived from an analysis of X-band marine radar images. Coastal Engineering 37: 513-527
  8. ↑ Greidanus, H. 1997. The use of radar for bathymetry in shallow seas. The Hydrographic Journal 83: 13–18
  9. ↑ Gawehn, M., van Dongeren, A., de Vries, S., Swinkels, C., Hoekstra, R., Aarninkhof, S. and Friedman, L. 2020. The application of a radar-based depth inversion method to monitor near-shore nourishments on an open sandy coast and an ebb-tidal delta. Coastal Engineering 159, 103716
  10. ↑ Almar, R., Bergsma, E.W., Thoumyre, G., Baba, M.W., Cesbron, G., Daly, C., Garlan, T. and Lifermann, A. 2021. Global satellite-based coastal bathymetry from waves. Remote Sensing 13, 4628
  11. ↑ Streßer, M., Carrasco, R. and Horstmann, J. 2017. Video-based estimation of surface currents using a low-cost quadcopter. Geosci. Rem. Sens. Lett. IEEE 14: 2027–2031
  12. ↑ Fairley, I., King, N., McIlvenny, J., Lewis, M., Neill, S., Williamson, B.J., Masters, I. and Reeve, D.E. 2024. Intercomparison of surface velocimetry techniques for drone-based marine current characterization. Estuarine, Coastal and Shelf Science 299, 108682


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 (2024): Bathymetry from remote sensing wave propagation. Available from http://www.coastalwiki.org/wiki/Bathymetry_from_remote_sensing_wave_propagation [accessed on 21-11-2024]
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