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to a relatively small neighborhood. Fluid moves upwards as the crest of the surface wave is passing and downwards as the trough passes. Lateral motion only serves to make up for the height difference in the water column between the crest and trough of the wave: as the surface rises at the top of the water column, water moves laterally inward from adjacent downwards-moving water columns to make up for the change in volume of the water column. While this explanation focuses on the motion of the ocean water, the phenomenon being described is in nature an interfacial wave, with mirroring processes happening on either side of the interface between two fluids: ocean water and air. At the simplest level, an internal wave can be thought of as an interfacial wave (Fig. 1, bottom) at the interface of two layers of the oceans differentiated by a change in the water's properties, such as a warm surface layer and cold deep layer separated by a thermocline. As the surface tide propagates between these two fluid layers at the ocean surface, a homologous internal wave mimics it below, forming the internal tide. The interfacial movement between two layers of ocean is large compared to surface movement because although as with surface waves, the restoring force for internal waves and tides is still gravity, its effect is reduced because the densities of the two layers are relatively similar compared to the large density difference at the air-sea interface. Thus larger displacements are possible inside the ocean than are possible at the sea surface.
150:
topography: âA number of lines of evidence, none complete, suggest that the oceanic general circulation, far from being a heat engine, is almost wholly governed by the forcing of the wind field and secondarily by deep water tides... The now inescapable conclusion that over most of the ocean significant âverticalâ mixing is confined to topographically complex boundary areas implies a potentially radically different interior circulation than is possible with uniform mixing. Whether ocean circulation models... neither explicitly accounting for the energy input into the system nor providing for spatial variability in the mixing, have any physical relevance under changed climate conditions is at issue.â There is a limited understanding of âthe sources controlling the internal wave energy in the ocean and the rate at which it is dissipatedâ and are only now developing some âparameterizations of the mixing generated by the interaction of internal waves,
87:
near-inertial wave generation, Garrett and Kunze (2007) observed 33 years later that âThe fate of the radiated is still uncertain. They may scatter into on further encounter with islands or the rough seafloor , or transfer their energy to smaller-scale internal waves in the ocean interior â or âbreak on distant continental slopes â. It is now known that most of the internal tide energy generated at tall, steep midocean topography radiates away as large-scale internal waves. This radiated internal tide energy is one of the main sources of energy into the deep ocean, roughly half of the wind energy input . Broader interest in internal tides is spurred by their impact on the magnitude and spatial inhomogeneity of mixing, which in turn has first order effect on the meridional overturning circulation .
65:
onshore and dissipate much like surface waves. Or internal tides may propagate away from the topography into the open ocean. For tall, steep, midocean topography, such as the
Hawaiian Ridge, it is estimated that about 85% of the energy in the internal tide propagates away into the deep ocean with about 15% of its energy being lost within about 50 km of the generation site. The lost energy contributes to turbulence and mixing near the generation sites. It is not clear where the energy that leaves the generation site is dissipated, but there are 3 possible processes: 1) the internal tides scatter and/or break at distant midocean topography, 2) interactions with other internal waves remove energy from the internal tide, or 3) the internal tides shoal and break on continental shelves.
116:. The energy flux at one point can be summed over depth- this is the depth-integrated energy flux and is measured in Watts/m. The Hawaiian Ridge produces depth-integrated energy fluxes as large as 10 kW/m. The longest wavelength waves are the fastest and thus carry most of the energy flux. Near Hawaii, the typical wavelength of the longest internal tide is about 150 km while the next longest is about 75 km. These waves are called mode 1 and mode 2, respectively. Although Fig. 1 shows there is no sea surface expression of the internal tide, there actually is a displacement of a few centimeters. These sea surface expressions of the internal tide at different wavelengths can be detected with the
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146:) redistributes about 2 PW of heat from the tropics to polar regions, the energy source for this flow is the interior mixing which is comparatively much smaller- about 2 TW. Sandstrom (1908) showed a fluid which is both heated and cooled at its surface cannot develop a deep overturning circulation. Most global models have incorporated uniform mixing throughout the ocean because they do not include or resolve internal tidal flows.
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82:.) The longest internal tide wavelengths are about 150 km near Hawaii and the next longest waves are about 75 km long. The surface displacements due to the internal tide are plotted as wiggly red lines with amplitudes plotted perpendicular to the satellite groundtracks (black lines). Figure is adapted from Johnston et al. (2003).
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The inescapable conclusion is that energy is lost from the surface tide to the internal tide at midocean topography and continental shelves, but the energy in the internal tide is not necessarily lost in the same place. Internal tides may propagate thousands of kilometers or more before breaking and
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The importance of internal tides and internal waves in general relates to their breaking, energy dissipation, and mixing of the deep ocean. If there were no mixing in the ocean, the deep ocean would be a cold stagnant pool with a thin warm surface layer. While the meridional overturning circulation
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in which water parcels in the whole water column oscillate in the same direction at a given phase (i.e., in the trough or at the crest, Fig. 1, top). This means that while the form of the surface wave itself may propagate across the surface of the water, the fluid particles themselves are restricted
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Internal tides may also dissipate on continental slopes and shelves or even reach within 100 m of the beach (Fig. 3). Internal tides bring pulses of cold water shoreward and produce large vertical temperature differences. When surface waves break, the cold water is mixed upwards, making the water
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Briscoe (1975)noted that âWe cannot yet answer satisfactorily the questions: âwhere does the internal wave energy come from, where does it go, and what happens to it along the way?ââ Although technological advances in instrumentation and modeling have produced greater knowledge of internal tide and
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The largest internal tides are generated at steep, midocean topography such as the
Hawaiian Ridge, Tahiti, the Macquarie Ridge, and submarine ridges in the Luzon Strait. Continental slopes such as the Australian North West Shelf also generate large internal tides. These internal tide may propagate
43:
Figure 1: Water parcels in the whole water column move together with the surface tide (top), while shallow and deep waters move in opposite directions in an internal tide (bottom). The surface displacement and interface displacement are the same for a surface wave (top), while for an internal wave
30:
at a tidal frequency. The other major source of internal waves is the wind which produces internal waves near the inertial frequency. When a small water parcel is displaced from its equilibrium position, it will return either downwards due to gravity or upwards due to buoyancy. The water parcel
77:
Figure 2: The internal tide sea surface elevation that is in phase with the surface tide (i.e., crests occur in a certain spot at a certain time that are both the same relative to the surface tide) can be detected by satellite (top). (The satellite track is repeated about every 10 days and so M2
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However, models are now beginning to include spatially variable mixing related to internal tides and the rough topography where they are generated and distant topography where they may break. Wunsch and
Ferrari (2004) describe the global impact of spatially inhomogeneous mixing near midocean
31:
will overshoot its original equilibrium position and this disturbance will set off an internal gravity wave. Munk (1981) notes, "Gravity waves in the ocean's interior are as common as waves at the sea surface-perhaps even more so, for no one has ever reported an interior calm."
124:
satellites (Fig. 2). Near 15 N, 175 W on the Line
Islands Ridge, the mode-1 internal tides scatter off the topography, possibly creating turbulence and mixing, and producing smaller wavelength mode 2 internal tides.
56:
Tides occur mainly at diurnal and semidiurnal periods. The principal lunar semidiurnal constituent is known as M2 and generally has the largest amplitudes. (See external links for more information.)
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Variabilidad temporal de la producciĂłn primaria fitoplanctonica en la estaciĂłn CaTS (Caribbean Time-Series
Station): Con Ă©nfasis en el impacto de la marea interna semidiurna sobre la producciĂłn
170:. The black line shows the surface tide elevation relative to mean lower low water (MLLW). Figure provided by Eric Terrill, Scripps Institution of Oceanography with funding from the U.S.
2013:
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Sharples, J.; V. Krivtsov; J. F. Tweddle; J. A. M. Green; M. R. Palmer; Y. Kim; A. E. Hickman; P. M. Holligan; C. M. Moore; T. P. Rippeth & J. H. Simpson (2007).
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The internal tidal energy in one tidal period going through an area perpendicular to the direction of propagation is called the energy flux and is measured in Watts/m
2003:
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the surface displacements are very small, while the interface displacements are large (bottom). This figure is a modified version of one appearing in Gill (1982).
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locally. Another mechanism for higher nitrate flux at spring tides results from pulses of strong turbulent dissipation associated with high frequency internal
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920:. Ph. D. Dissertation. Department of Marine Sciences, University of Puerto Rico, MayagĂŒez, Puerto Rico. UMI publication AAT 3042382. p. 407
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Carter, G. S.; Y. L. Firing; M. A. Merrifield; J. M. Becker; K. Katsumata; M. C. Gregg; D. S. Luther; M. D. Levine & T. J. Boyd (2008).
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cold for surfers, swimmers, and other beachgoers. Surface waters in the surf zone can change by about 10 °C in about an hour.
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Klymak, J. M.; M. C. Gregg; J. N. Moum; J. D. Nash; E. Kunze; J. B. Girton; G. S. Carter; C. M. Lee & T. B. Sanford (2006).
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during the breaking of the internal tide can explain the formation of high diffusivity patches that generate a vertical flux of
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190:, or near the shelf edge, can enhance turbulent dissipation and internal mixing near the generation site. The development of
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move stratified water up and down sloping topography, which produces a wave in the ocean interior. So internal tides are
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Simmons, H. L.; B. K. Arbic & R. W. Hallberg (2004). "Internal wave generation in a global baroclinic tide model".
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Internal tides generated by tidal semidiurnal currents impinging on steep submarine ridges in island passages, ex:
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940:"Internal Tide-induced Variations in Primary Productivity and Optical Properties in the Mona Passage, Puerto Rico"
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Figure 3: The internal tide produces large vertical differences in temperature at the research pier at the
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packets. Some internal soliton packets are the result of the nonlinear evolution of the internal tide.
968:"Springâneap modulation of internal tide mixing and vertical nitrate fluxes at a shelf edge in summer"
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Wunsch, C.; R. Ferrari (2004). "Vertical mixing, energy, and the general circulation of the ocean".
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Briscoe, M. (1975). "Introduction to a collection of papers on oceanographic internal waves".
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Munk, W. (1981). B. A. Warren; C. Wunsch (eds.). "Internal Waves and Small-Scale
Processes".
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Munk, W.; Wunsch, C. (1998). "Abyssal recipes II: Energetics of tidal and wind mixing".
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154:, high-frequency barotropic fluctuations, and other motions over sloping topography.â
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638:"Subtropical catastrophe: Significant loss of low-mode tidal energy at 28.9 degrees"
393:"Energetics of M2 Barotropic-to-Baroclinic Tidal Conversion at the Hawaiian Islands"
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Alfonso-Sosa, E.; J. Morell; J. M. Lopez; J. E. Capella & A. Dieppa (2002).
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Principal tidal constituents in
Physical oceanography textbook, Bob Stewart of
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352:"A regional model of the semidiurnal tide on the Australian North West Shelf"
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Garrett, C.; E. Kunze (2007). "Internal tide generation in the deep ocean".
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690:"Internal tide reflection and turbulent mixing on the continental slope"
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434:"An Estimate of Tidal Energy Lost to Turbulence at the Hawaiian Ridge"
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Eric Kunze's work on internal waves, internal tides, mixing, and more
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1985:
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Johnston, T. M. S.; P. E. Holloway & M. A. Merrifield (2003).
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Internal Tides of the Oceans, Harper
Simmons, by Jenn Wagaman of
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223:
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Sandstrom, J. W. (1908). "Dynamische
Versuche mit Meerwasser".
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Nash, J. D.; R.W. Schmitt; E. Kunze & J.M. Toole (2004).
1035:
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10.1175/1520-0485(2004)034<1117:ITRATM>2.0.CO;2
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10.1175/1520-0485(2002)032<2882:TROITI>2.0.CO;2
510:"Internal tide scattering at seamounts, ridges and islands"
182:
Internal tides, internal mixing, and biological enhancement
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589:"The Role of Internal Tides in Mixing the Deep Ocean"
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Abyssal mixing and meridional overturning circulation
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552:"Internal tide scattering at the Line Islands Ridge"
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78:tidal signals are shifted to longer periods due to
1016:Southern California Coastal Ocean Observing System
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2014:North West Shelf Operational Oceanographic System
2004:Deep-ocean Assessment and Reporting of Tsunamis
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508:Johnston, T. M. S.; M. A. Merrifield (2003).
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636:MacKinnon, J. A.; K. B. Winters (2005).
587:St. Laurent; L. C.; C. Garrett (2002).
244:
1335:one-dimensional Saint-Venant equations
809:10.1146/annurev.fluid.36.050802.122121
759:10.1146/annurev.fluid.39.050905.110227
7:
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857:Munk, W. (1966). "Abyssal recipes".
1023:Arctic Region Supercomputing Center
1011:Scripps Institution of Oceanography
168:Scripps Institution of Oceanography
2162:National Oceanographic Data Center
1589:World Ocean Circulation Experiment
1477:Global Ocean Data Analysis Project
254:Evolution of Physical Oceanography
14:
2009:Global Sea Level Observing System
894:Ann. Hydrodyn. Marine Meteorology
48:The surface tide propagates as a
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1467:Geochemical Ocean Sections Study
1383:
1372:
2197:Ocean thermal energy conversion
1920:VineâMatthewsâMorley hypothesis
558:. 108. (C11) 3365 (C11): 3365.
16:Wave within the ocean interior
1:
844:10.1016/S0967-0637(98)00070-3
516:. 108. (C6) 3126 (C6): 3180.
22:are generated as the surface
1457:El NiñoâSouthern Oscillation
1427:CraikâLeibovich vortex force
1183:Luke's variational principle
879:10.1016/0011-7471(66)90602-4
192:Kelvin-Helmholtz instability
158:Internal tides at the beach
69:Propagation and dissipation
2341:
1522:Ocean dynamical thermostat
1370:
337:10.1016/j.dsr2.2004.09.015
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2057:Ocean acoustic tomography
1870:MohoroviÄiÄ discontinuity
1462:General circulation model
1098:BenjaminâFeir instability
993:10.4319/lo.2007.52.5.1735
907:Alfonso-Sosa, E. (2002).
307:Deep-Sea Research Part II
274:Atmosphere-ocean dynamics
142:(also referred to as the
2187:Ocean surface topography
1562:Thermohaline circulation
1552:Subsurface ocean current
1492:Hydrothermal circulation
1325:Waveâcurrent interaction
1103:Boussinesq approximation
1031:Texas A&M University
350:Holloway, P. E. (2001).
172:Office of Naval Research
144:thermohaline circulation
2224:Sea surface temperature
2207:Outline of oceanography
1402:Atmospheric circulation
1340:shallow water equations
1330:Waves and shallow water
1223:Significant wave height
495:10.1029/JC080i003p00289
362:(C9): 19, 625â19, 638.
2219:Sea surface microlayer
1584:Wind generated current
174:
110:
83:
45:
2325:Physical oceanography
2052:Deep scattering layer
2034:World Geodetic System
1542:Princeton Ocean Model
1422:CoriolisâStokes force
1072:Physical oceanography
779:Annu. Rev. Fluid Mech
739:Annu. Rev. Fluid Mech
418:10.1175/2008JPO3860.1
277:. Academic. pp.
234:Physical oceanography
165:
111:
76:
42:
2072:Underwater acoustics
1632:Perigean spring tide
1497:Langmuir circulation
1208:Rossby-gravity waves
663:10.1029/2005GL023376
573:10.1029/2003JC001844
531:10.1029/2002JC001528
377:10.1029/2000jc000675
313:(25â26): 3043â3068.
271:Gill, A. E. (1982).
109:{\displaystyle ^{2}}
94:
2234:Science On a Sphere
1840:Convergent boundary
1512:Modular Ocean Model
1472:Geostrophic current
1188:Mild-slope equation
984:2007LimOc..52.1735S
871:1966DSRA...13..707M
836:1998DSRI...45.1977M
791:2004AnRFM..36..281W
751:2007AnRFM..39...57G
706:2004JPO....34.1117N
654:2005GeoRL..3215605M
605:2002JPO....32.2882S
564:2003JGRC..108.3365J
522:2003JGRC..108.3180J
487:1975JGR....80..289B
450:2006JPO....36.1148K
409:2008JPO....38.2205C
368:2001JGR...10619625H
319:2004DSRII..51.3043S
1890:Seafloor spreading
1880:Outer trench swell
1845:Divergent boundary
1745:Continental margin
1730:Carbonate platform
1627:Lunitidal interval
642:Geophys. Res. Lett
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106:
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35:Simple explanation
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2299:Oceans portal
2259:World Ocean Atlas
2249:Underwater glider
2192:Ocean temperature
1855:Hydrothermal vent
1820:Submarine volcano
1755:Continental shelf
1735:Coastal geography
1725:Bathymetric chart
1607:Amphidromic point
1295:Wave nonlinearity
1153:Infragravity wave
859:Deep-Sea Research
830:(12): 1977â2010.
824:Deep-Sea Research
694:J. Phys. Oceanogr
599:(10): 2882â2899.
593:J. Phys. Oceanogr
459:10.1175/JPO2885.1
438:J. Phys. Oceanogr
403:(10): 2205â2223.
397:J. Phys. Oceanogr
288:978-0-12-283522-3
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2152:Marine pollution
1946:Deep ocean water
1815:Submarine canyon
1750:Continental rise
1642:Rule of twelfths
1557:Sverdrup balance
1487:Humboldt Current
1412:Boundary current
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1193:Radiation stress
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1138:Equatorial waves
1093:Ballantine scale
1088:Airy wave theory
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978:(5): 1735â1747.
972:Limnol. Oceanogr
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1682:Tidal resonance
1652:Theory of tides
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1502:Longshore drift
1452:Ekman transport
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220:
201:
184:
160:
139:
97:
92:
91:
71:
62:
37:
17:
12:
11:
5:
2338:
2336:
2328:
2327:
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2305:
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2301:
2289:
2279:
2268:
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2256:
2251:
2246:
2241:
2239:Stratification
2236:
2231:
2226:
2221:
2216:
2211:
2210:
2209:
2199:
2194:
2189:
2184:
2179:
2174:
2169:
2164:
2159:
2154:
2149:
2144:
2139:
2131:
2129:Color of water
2126:
2124:Benthic lander
2121:
2116:
2110:
2108:
2104:
2103:
2101:
2100:
2095:
2090:
2084:
2082:
2078:
2077:
2075:
2074:
2069:
2064:
2059:
2054:
2048:
2046:
2040:
2039:
2037:
2036:
2031:
2029:Sea level rise
2026:
2024:Sea level drop
2021:
2016:
2011:
2006:
2000:
1998:
1992:
1991:
1989:
1988:
1983:
1978:
1973:
1968:
1963:
1958:
1953:
1948:
1943:
1937:
1935:
1931:
1930:
1928:
1927:
1922:
1917:
1912:
1907:
1902:
1897:
1892:
1887:
1882:
1877:
1872:
1867:
1862:
1860:Marine geology
1857:
1852:
1847:
1842:
1836:
1834:
1826:
1825:
1823:
1822:
1817:
1812:
1807:
1802:
1800:Passive margin
1797:
1795:Oceanic trench
1792:
1787:
1782:
1777:
1772:
1767:
1762:
1757:
1752:
1747:
1742:
1737:
1732:
1727:
1722:
1717:
1712:
1706:
1704:
1698:
1697:
1695:
1694:
1689:
1684:
1679:
1674:
1669:
1664:
1659:
1654:
1649:
1644:
1639:
1634:
1629:
1624:
1619:
1614:
1609:
1603:
1601:
1595:
1594:
1592:
1591:
1586:
1581:
1576:
1571:
1570:
1569:
1559:
1554:
1549:
1544:
1539:
1534:
1529:
1527:Ocean dynamics
1524:
1519:
1514:
1509:
1504:
1499:
1494:
1489:
1484:
1479:
1474:
1469:
1464:
1459:
1454:
1449:
1444:
1439:
1434:
1429:
1424:
1419:
1417:Coriolis force
1414:
1409:
1404:
1398:
1396:
1390:
1389:
1371:
1369:
1367:
1366:
1365:
1364:
1354:
1349:
1344:
1343:
1342:
1337:
1327:
1322:
1317:
1312:
1307:
1302:
1297:
1292:
1287:
1282:
1277:
1272:
1267:
1266:
1265:
1255:
1250:
1245:
1240:
1238:Stokes problem
1235:
1230:
1225:
1220:
1215:
1210:
1205:
1200:
1195:
1190:
1185:
1180:
1175:
1173:Kinematic wave
1170:
1165:
1160:
1155:
1150:
1145:
1140:
1135:
1130:
1125:
1120:
1115:
1110:
1105:
1100:
1095:
1090:
1084:
1082:
1076:
1075:
1070:
1068:
1067:
1060:
1053:
1045:
1039:
1038:
1033:
1025:
1017:
1012:
1005:
1004:External links
1002:
1000:
999:
958:
930:
899:
884:
865:(4): 707â730.
849:
814:
785:(1): 281â314.
764:
729:
677:
648:(15): L15605.
628:
579:
537:
500:
481:(3): 289â290.
465:
424:
383:
342:
294:
287:
263:
243:
241:
238:
237:
236:
231:
226:
219:
216:
208:new production
199:
183:
180:
159:
156:
138:
135:
118:Topex/Poseidon
103:
99:
70:
67:
61:
58:
36:
33:
28:internal waves
20:Internal tides
15:
13:
10:
9:
6:
4:
3:
2:
2337:
2326:
2323:
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2318:
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2315:
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2270:
2269:
2266:
2260:
2257:
2255:
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2222:
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2160:
2158:
2155:
2153:
2150:
2148:
2147:Marine energy
2145:
2143:
2140:
2138:
2137:
2132:
2130:
2127:
2125:
2122:
2120:
2117:
2115:
2114:Acidification
2112:
2111:
2109:
2105:
2099:
2096:
2094:
2091:
2089:
2086:
2085:
2083:
2079:
2073:
2070:
2068:
2067:SOFAR channel
2065:
2063:
2060:
2058:
2055:
2053:
2050:
2049:
2047:
2045:
2041:
2035:
2032:
2030:
2027:
2025:
2022:
2020:
2017:
2015:
2012:
2010:
2007:
2005:
2002:
2001:
1999:
1997:
1993:
1987:
1984:
1982:
1979:
1977:
1974:
1972:
1969:
1967:
1964:
1962:
1959:
1957:
1954:
1952:
1949:
1947:
1944:
1942:
1939:
1938:
1936:
1932:
1926:
1923:
1921:
1918:
1916:
1913:
1911:
1908:
1906:
1903:
1901:
1898:
1896:
1893:
1891:
1888:
1886:
1883:
1881:
1878:
1876:
1875:Oceanic crust
1873:
1871:
1868:
1866:
1863:
1861:
1858:
1856:
1853:
1851:
1850:Fracture zone
1848:
1846:
1843:
1841:
1838:
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1835:
1833:
1827:
1821:
1818:
1816:
1813:
1811:
1808:
1806:
1803:
1801:
1798:
1796:
1793:
1791:
1788:
1786:
1785:Oceanic basin
1783:
1781:
1778:
1776:
1773:
1771:
1768:
1766:
1763:
1761:
1758:
1756:
1753:
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1748:
1746:
1743:
1741:
1738:
1736:
1733:
1731:
1728:
1726:
1723:
1721:
1718:
1716:
1715:Abyssal plain
1713:
1711:
1708:
1707:
1705:
1703:
1699:
1693:
1690:
1688:
1685:
1683:
1680:
1678:
1675:
1673:
1670:
1668:
1665:
1663:
1660:
1658:
1655:
1653:
1650:
1648:
1645:
1643:
1640:
1638:
1635:
1633:
1630:
1628:
1625:
1623:
1622:Internal tide
1620:
1618:
1615:
1613:
1610:
1608:
1605:
1604:
1602:
1600:
1596:
1590:
1587:
1585:
1582:
1580:
1577:
1575:
1572:
1568:
1565:
1564:
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1560:
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1555:
1553:
1550:
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1543:
1540:
1538:
1535:
1533:
1530:
1528:
1525:
1523:
1520:
1518:
1517:Ocean current
1515:
1513:
1510:
1508:
1505:
1503:
1500:
1498:
1495:
1493:
1490:
1488:
1485:
1483:
1480:
1478:
1475:
1473:
1470:
1468:
1465:
1463:
1460:
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1455:
1453:
1450:
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1440:
1438:
1435:
1433:
1430:
1428:
1425:
1423:
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1413:
1410:
1408:
1405:
1403:
1400:
1399:
1397:
1395:
1391:
1386:
1375:
1363:
1360:
1359:
1358:
1355:
1353:
1350:
1348:
1345:
1341:
1338:
1336:
1333:
1332:
1331:
1328:
1326:
1323:
1321:
1318:
1316:
1315:Wave shoaling
1313:
1311:
1308:
1306:
1303:
1301:
1298:
1296:
1293:
1291:
1288:
1286:
1283:
1281:
1278:
1276:
1275:Ursell number
1273:
1271:
1268:
1264:
1261:
1260:
1259:
1256:
1254:
1251:
1249:
1246:
1244:
1241:
1239:
1236:
1234:
1231:
1229:
1226:
1224:
1221:
1219:
1216:
1214:
1211:
1209:
1206:
1204:
1201:
1199:
1196:
1194:
1191:
1189:
1186:
1184:
1181:
1179:
1176:
1174:
1171:
1169:
1166:
1164:
1161:
1159:
1158:Internal wave
1156:
1154:
1151:
1149:
1146:
1144:
1141:
1139:
1136:
1134:
1131:
1129:
1126:
1124:
1121:
1119:
1116:
1114:
1111:
1109:
1108:Breaking wave
1106:
1104:
1101:
1099:
1096:
1094:
1091:
1089:
1086:
1085:
1083:
1081:
1077:
1073:
1066:
1061:
1059:
1054:
1052:
1047:
1046:
1043:
1036:
1034:
1032:
1028:
1026:
1024:
1020:
1018:
1015:
1013:
1010:
1008:
1007:
1003:
994:
989:
985:
981:
977:
973:
969:
962:
959:
946:
941:
934:
931:
917:
912:
911:
903:
900:
895:
888:
885:
880:
876:
872:
868:
864:
860:
853:
850:
845:
841:
837:
833:
829:
825:
818:
815:
810:
806:
801:
796:
792:
788:
784:
780:
773:
771:
769:
765:
760:
756:
752:
748:
744:
740:
733:
730:
725:
721:
716:
711:
707:
703:
699:
695:
691:
684:
682:
678:
673:
669:
664:
659:
655:
651:
647:
643:
639:
632:
629:
624:
620:
615:
610:
606:
602:
598:
594:
590:
583:
580:
574:
569:
565:
561:
557:
553:
546:
544:
542:
538:
532:
527:
523:
519:
515:
511:
504:
501:
496:
492:
488:
484:
480:
476:
469:
466:
460:
455:
451:
447:
443:
439:
435:
428:
425:
419:
414:
410:
406:
402:
398:
394:
387:
384:
378:
373:
369:
365:
361:
357:
353:
346:
343:
338:
334:
329:
324:
320:
316:
312:
308:
301:
299:
295:
290:
284:
280:
276:
275:
267:
264:
259:
255:
248:
245:
239:
235:
232:
230:
229:Internal wave
227:
225:
222:
221:
217:
215:
213:
209:
205:
197:
193:
189:
181:
179:
173:
169:
164:
157:
155:
153:
147:
145:
136:
134:
132:
126:
123:
119:
101:
98:
88:
81:
75:
68:
66:
59:
57:
54:
51:
41:
34:
32:
29:
25:
21:
2254:Water column
2202:Oceanography
2177:Observations
2172:Explorations
2142:Marginal sea
2135:
2093:OSTM/Jason-2
1925:Volcanic arc
1900:Slab suction
1621:
1617:Head of tide
1507:Loop Current
1447:Ekman spiral
1233:Stokes drift
1143:Gravity wave
1118:Cnoidal wave
975:
971:
961:
950:. Retrieved
933:
922:. Retrieved
909:
902:
893:
887:
862:
858:
852:
827:
823:
817:
782:
778:
745:(1): 57â87.
742:
738:
732:
697:
693:
645:
641:
631:
596:
592:
582:
555:
513:
503:
478:
474:
468:
441:
437:
427:
400:
396:
386:
359:
355:
345:
310:
306:
273:
266:
253:
247:
188:Mona Passage
185:
176:
148:
140:
127:
89:
85:
63:
55:
47:
19:
18:
2244:Thermocline
1961:Mesopelagic
1934:Ocean zones
1905:Slab window
1770:Hydrography
1710:Abyssal fan
1677:Tidal range
1667:Tidal power
1662:Tidal force
1547:Rip current
1482:Gulf Stream
1442:Ekman layer
1432:Downwelling
1407:Baroclinity
1394:Circulation
1290:Wave height
1280:Wave action
1263:megatsunami
1243:Stokes wave
1203:Rossby wave
1168:Kelvin wave
1148:Green's law
204:photic zone
202:) into the
129:mixing the
2314:Categories
2182:Reanalysis
2081:Satellites
2062:Sofar bomb
1910:Subduction
1885:Ridge push
1780:Ocean bank
1760:Contourite
1687:Tide gauge
1672:Tidal race
1657:Tidal bore
1647:Slack tide
1612:Earth tide
1532:Ocean gyre
1352:Wind setup
1347:Wind fetch
1310:Wave setup
1305:Wave radar
1300:Wave power
1198:Rogue wave
1128:Dispersion
952:2015-01-01
924:2014-08-25
260:: 264â291.
240:References
2044:Acoustics
1996:Sea level
1895:Slab pull
1832:tectonics
1740:Cold seep
1702:Landforms
1579:Whirlpool
1574:Upwelling
1357:Wind wave
1285:Wave base
1213:Sea state
1133:Edge wave
1123:Cross sea
795:CiteSeerX
724:1520-0485
623:1520-0485
323:CiteSeerX
258:MIT Press
2277:Category
2229:Seawater
1956:Littoral
1951:Deep sea
1810:Seamount
1692:Tideline
1637:Rip tide
1567:shutdown
1537:Overflow
1270:Undertow
1113:Clapotis
672:54573466
218:See also
80:aliasing
60:Location
2287:Commons
2157:Mooring
2107:Related
2098:Jason-3
2088:Jason-1
1971:Pelagic
1966:Oceanic
1941:Benthic
1258:Tsunami
1228:Soliton
980:Bibcode
867:Bibcode
832:Bibcode
787:Bibcode
747:Bibcode
702:Bibcode
650:Bibcode
601:Bibcode
560:Bibcode
518:Bibcode
483:Bibcode
446:Bibcode
405:Bibcode
364:Bibcode
315:Bibcode
212:soliton
196:nitrate
133:ocean.
131:abyssal
122:Jason-1
1976:Photic
1805:Seabed
1218:Seiche
797:
722:
670:
621:
325:
285:
2320:Tides
2167:Ocean
2136:Alvin
1986:Swash
1830:Plate
1775:Knoll
1765:Guyot
1720:Atoll
1599:Tides
1362:model
1248:Swell
1080:Waves
668:S2CID
24:tides
2134:DSV
2119:Argo
1981:Surf
1437:Eddy
896:: 6.
720:ISSN
619:ISSN
283:ISBN
224:Tide
50:wave
988:doi
945:PDF
916:PDF
875:doi
840:doi
805:doi
755:doi
710:doi
658:doi
609:doi
568:doi
526:doi
491:doi
454:doi
413:doi
372:doi
360:106
333:doi
279:662
198:(NO
120:or
2316::
986:.
976:52
974:.
970:.
873:.
863:13
861:.
838:.
828:45
826:.
803:.
793:.
783:36
781:.
767:^
753:.
743:39
741:.
718:.
708:.
698:34
696:.
692:.
680:^
666:.
656:.
646:32
644:.
640:.
617:.
607:.
597:32
595:.
591:.
566:.
554:.
540:^
524:.
512:.
489:.
479:80
477:.
452:.
442:36
440:.
436:.
411:.
401:38
399:.
395:.
370:.
358:.
354:.
331:.
321:.
311:51
309:.
297:^
281:.
256:.
1064:e
1057:t
1050:v
996:.
990::
982::
955:.
947:)
943:(
927:.
918:)
914:(
881:.
877::
869::
846:.
842::
834::
811:.
807::
789::
761:.
757::
749::
726:.
712::
704::
674:.
660::
652::
625:.
611::
603::
576:.
570::
562::
534:.
528::
520::
497:.
493::
485::
462:.
456::
448::
421:.
415::
407::
380:.
374::
366::
339:.
335::
317::
291:.
200:3
102:2
Text is available under the Creative Commons Attribution-ShareAlike License. Additional terms may apply.
