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{{Short description|Enhanced tide due to ocean resonance}}
[[Image:PortisheadDocks_NearHighTide.JPG|thumb|200px|right|alt High tide at Portishead Docks in the Bristol Channel.|]]
{{About|the oceanography phenomenon|usage in astronomy|Tidal locking}}
[[Image:PortisheadDocks_LowTide.JPG|thumb|200px|right|alt=Low tide at Portishead Docks in the Bristol Channel. Such extreme tidal ranges are almost certainly due to resonant waves tapped between the coast and the edge of the continental shelf.|High and tow tides at Portishead Docks in the Bristol Channel. Such extreme tidal ranges (13 m) are almost certainly due to a resonant tidal wave trapped between the coast and the edge of the continental shelf.]]
 
[[File:PortisheadDocks Tides.JPG|thumb|upright=1.5|Tides at [[Portishead, Somerset|Portishead]] Dock in the Bristol Channel. An example of tidal resonance.]]
 
In [[oceanography]], a '''tidal [[resonance]]''' occurs when the [[tide]] excites one of the [[resonance|resonant]] modes of the ocean.<ref name=Platzman91>
<ref name=Platzman91>▼
{{Citation
| last = Platzman
| first = G.W.
| yeardate = 1991
| contribution = Tidal Evidence for Ocean Normal Modes
| editor-last = Parker
| editor-first = B.P.
| title = Tidal Hydrodynamics
| publication-placelocation = New York
| publisher = [[John Wiley & Sons]]
| pages = 883
}}</ref>.
The effect is most striking when a [[continental shelf]] is about a quarter wavelength wide. Then an incident tidal wave can be reinforced by reflections between the coast and the shelf edge, the result producing a much higher [[tidal range]] at the coast.
 
Famous examples of this effect are found in the [[Bay of Fundy]], where the world's highest tides are reportedly found, and in the [[Bristol Channel]]. LargeLess tideswell dueknown tois resonancesLeaf areBay, alsopart foundof on[[Ungava Bay]] near the Patagonianentrance of [[Hudson Strait]] ([[Canada]]), which has tides similar to those of the [[Bay of Fundy]].<ref Shelfname=OReilly2005>
{{Cite journal
<ref name=Webb76>
| last = O'Reilly
| first = C.T.
|author2=Solvason, R. |author3=Solomon, C.
| title = Where are the World's Largest Tides
| journal = BIO Annual Report: 2004 in Review
| editor = J. Ryan
| publisher=Biotechnol. Ind. Org., Washington, D. C.
| pages = 44–46
| date = 2005
}}</ref> Other resonant regions with large tides include the [[Patagonian Shelf]] and on the continental shelf of [[northwest Australia]].<ref name=Webb76>
{{Cite journal
| last = Webb
Line 26 ⟶ 36:
| title = A Model of Continental-shelf Resonances
| journal = Deep-Sea Research
| volume = 2523
| pagesissue = 1-15
| pages = 1–15
| date = 1976
| doi = 10.1016/0011-7471(76)90804-4
}}</ref>▼
| bibcode = 1976DSRA...23....1W
and on the N.W. Australian continental shelf.
▲ }}</ref>
 
Most of the resonant regions are also responsible for large fractions of the total amount of tidal energy dissipated in the oceans. Satellite altimeter data shows that the M<sub>2</sub> tide dissipates approximately 2.5&nbsp;TW, of which 261&nbsp;GW is lost in the [[Hudson Bay]] complex, 208&nbsp;GW on the European Shelves (including the Bristol Channel), 158&nbsp;GW on the North-west Australian Shelf, 149&nbsp;GW in the [[Yellow Sea]] and 112&nbsp;GW on the [[Patagonian Shelf]].<ref name=Egbert01>
{{cite journal
| last = Egbert
| first = G.D.
|author2= Ray, R.
| title = Estimates of M<sub>2</sub> tidal dissipation from TOPEX/Poseidon altimeter data
| journal = Journal of Geophysical Research
| volume = 106 (C10)
| pages = 22475–22502
| date = 2001
| issue = C10
|bibcode = 2001JGR...10622475E |doi = 10.1029/2000JC000699 | s2cid = 76652654
| doi-access = free}}</ref>
 
==Scale of the resonances==
The speed of long [[water waves|waves]] in the ocean is given, to a good approximation, by <math>\scriptstyle\sqrt{ghg h}</math>, where ''g'' is the acceleration of gravity and ''h'' is the depth of the ocean.<ref name=Segar07>
<ref name=Segar07>
{{Cite book
| last = Segar
Line 42 ⟶ 68:
| location = New York
| pages = 581+
}}</ref>
</ref><ref name=Knauss97>
{{Cite book
| last = Knauss
Line 52 ⟶ 78:
| location = Long Grove, USA
| pages = 309
}}</ref>
</ref><ref name=Defant61>
{{Cite book
| last = Defant
| first = A.
| title = Introduction to Physical Oceanography, Vol. II
| volume = II
| publisher = [[Pergamon Press]]
| date = 1961
| location = Oxford
| pages = 598
}}</ref>.
For a typical continental shelf with a depth of 100 &nbsp;m, the speed is approximately 30 &nbsp;m/s. So if the tidal period is 12 &nbsp;hours, a quarter wavelength shelf will have a width of about 300&nbsp;km.
 
With a narrower shelf, there is still a resonance but it is mismatched to the frequency of the tides and so has less effect aton tidal frequenciesamplitudes. However the effect is still enough to partly explain why tides along a coast lying behind a continental shelf are often higher than at offshore islands in the deep ocean (one of the additional partial explanations being [[Green's law]]). Resonances also Thegenerate strong tidal currents associatedand withit resonancesis alsothe meanturbulence thatcaused by the resonantcurrents regionswhich areis responsible for the areaslarge whereamount mostof tidal energy is dissipated in such regions.
 
In the deep ocean, where the depth is typically 4000 &nbsp;m, the speed of long waves increases to approximately 200 &nbsp;m/s. The difference in speed, when compared to the shelf, is responsible for the reflections at the continental shelf edge. Away from resonance this can stopreduce tidal energy moving onto the shelf. However near a resonant frequency the phase relationshipsrelationship, between the wavewaves on the shelf and in the deep ocean, can have the effect of drawing energy onto the shelf.
 
The increased speed of long waves in the deep ocean means that the tidal wavelength there is of order 10,000&nbsp;km. As the ocean basins have a similar size, they also have the potential of being resonant.<ref name=Platzman81>
<ref name=Platzman81>
{{Cite journal
| last = Platzman
| first = G.W.
| coauthors author2= Curtis, G.A., |author3=Hansen, K.S., |author4=Slater, R.D.
| title = Normal Modes of the World ocean. Part II: Description of Modes in the Period Range 8 to 80 Hours
| journal = [[Journal of Physical Oceanography]]
| volume = 11
| issue = 5
| pages = 579-603579–603
| date = 1981
|bibcode = 1981JPO....11..579P |doi = 10.1175/1520-0485(1981)011<0579:NMOTWO>2.0.CO;2 | doi-access = free
}}</ref>▼
}}
<ref name=Webb73>
▲</ref><ref name=Platzman91Webb73>
{{Cite journal
| last = Webb
| first = D.J.
| title = Tidal Resonance in the Coral Sea
| journal = [[Nature (journal) | Nature ]]
| volume = 243
| issue = 5409
| pages = 511
| date = 1973
|bibcode = 1973Natur.243..511W |doi = 10.1038/243511a0 | doi-access = free
}}</ref>.
▲ }}</ref>
In practice deep ocean resonances are difficult to observe, probably because the deep ocean loses tidal energy too rapidly to the resonant shelves.
 
==Tidal locking==
The above concept of tidal resonance differs from another sort of [[resonance]] resulting from tides, called [[tidal locking]], which causes a [[moon]]'s rotational period to coincide with the period of its revolution around the planet that it orbits, so that one side of the moon always faces the planet.
 
==See also==
Line 106 ⟶ 131:
==References==
 
{{Reflist}}
<references />
 
{{physical oceanography}}
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[[Category:Physical oceanography]]
[[Category:Tides]]
 
[[de:Tideresonanz]]
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