Theory of tides

High and low tide in the Bay of Fundy

The theory of tides is the application of continuum mechanics to interpret and predict the tidal deformations of planetary and satellite bodies and their atmospheres and oceans (especially Earth's oceans) under the gravitational loading of another astronomical body or bodies (especially the Moon and Sun).

History

Australian Aboriginal astronomy

The Yolngu people of northeastern Arnhem Land in the Northern Territory of Australia identified a link between the Moon and the tides, which they mythically attributed to the Moon filling with water and emptying out again.

Classical era

The tides received relatively little attention in the civilizations around the Mediterranean Sea, as the tides there are relatively small, and the areas that experience tides do so unreliably. A number of theories were advanced, however, from comparing the movements to breathing or blood flow to theories involving whirlpools or river cycles. A similar "breathing earth" idea was considered by some Asian thinkers. Plato reportedly believed that the tides were caused by water flowing in and out of undersea caverns. Crates of Mallus attributed the tides to "the counter-movement (ἀντισπασμός) of the sea” and Apollodorus of Corcyra to "the refluxes from the Ocean". An ancient Indian Purana text dated to 400-300 BC refers to the ocean rising and falling because of heat expansion from the light of the Moon.

Ultimately the link between the Moon (and Sun) and the tides became known to the Greeks, although the exact date of discovery is unclear; references to it are made in sources such as Pytheas of Massilia in 325 BC and Pliny the Elder's Natural History in 77 AD. Although the schedule of the tides and the link to lunar and solar movements was known, the exact mechanism that connected them was unclear. Classicists Thomas Little Heath claimed that both Pytheas and Posidonius connected the tides with the moon, "the former directly, the latter through the setting up of winds". Seneca mentions in De Providentia the periodic motion of the tides controlled by the lunar sphere. Eratosthenes (3rd century BC) and Posidonius (1st century BC) both produced detailed descriptions of the tides and their relationship to the phases of the Moon, Posidonius in particular making lengthy observations of the sea on the Spanish coast, although little of their work survived. The influence of the Moon on tides was mentioned in Ptolemy's Tetrabiblos as evidence of the reality of astrology. Seleucus of Seleucia is thought to have theorized around 150 BC that tides were caused by the Moon as part of his heliocentric model.

Aristotle, judging from discussions of his beliefs in other sources, is thought to have believed the tides were caused by winds driven by the Sun's heat, and he rejected the theory that the Moon caused the tides. An apocryphal legend claims that he committed suicide in frustration with his failure to fully understand the tides. Heraclides also held "the sun sets up winds, and that these winds, when they blow, cause the high tide and, when they cease, the low tide". Dicaearchus also "put the tides down to the direct action of the sun according to its position". Philostratus discusses tides in Book Five of Life of Apollonius of Tyana (circa 217-238 AD); he was vaguely aware of a correlation of the tides with the phases of the Moon but attributed them to spirits moving water in and out of caverns, which he connected with the legend that spirits of the dead cannot move on at certain phases of the Moon.

Medieval period

The Venerable Bede discusses the tides in The Reckoning of Time and shows that the twice-daily timing of tides is related to the Moon and that the lunar monthly cycle of spring and neap tides is also related to the Moon's position. He goes on to note that the times of tides vary along the same coast and that the water movements cause low tide at one place when there is high tide elsewhere. However, he made no progress regarding the question of how exactly the Moon created the tides.

Medieval rule-of-thumb methods for predicting tides were said to allow one "to know what Moon makes high water" from the Moon's movements. Dante references the Moon's influence on the tides in his Divine Comedy.

Medieval European understanding of the tides was often based on works of Muslim astronomers that became available through Latin translation starting from the 12th century. Abu Ma'shar al-Balkhi, in his Introductorium in astronomiam, taught that ebb and flood tides were caused by the Moon. Abu Ma'shar discussed the effects of wind and Moon's phases relative to the Sun on the tides. In the 12th century, al-Bitruji contributed the notion that the tides were caused by the general circulation of the heavens. Medieval Arabic astrologers frequently referenced the Moon's influence on the tides as evidence for the reality of astrology; some of their treatises on the topic influenced western Europe. Some theorized that the influence was caused by lunar rays heating the ocean's floor.

Modern era

Simon Stevin in his 1608 De spiegheling der Ebbenvloet (The Theory of Ebb and Flood) dismisses a large number of misconceptions that still existed about ebb and flood. Stevin pleads for the idea that the attraction of the Moon was responsible for the tides and writes in clear terms about ebb, flood, spring tide and neap tide, stressing that further research needed to be made. In 1609, Johannes Kepler correctly suggested that the gravitation of the Moon causes the tides, which he compared to magnetic attraction basing his argument upon ancient observations and correlations.

In 1616, Galileo Galilei wrote Discourse on the Tides. He strongly and mockingly rejects the lunar theory of the tides, and tries to explain the tides as the result of the Earth's rotation and revolution around the Sun, believing that the oceans moved like water in a large basin: as the basin moves, so does the water. Therefore, as the Earth revolves, the force of the Earth's rotation causes the oceans to "alternately accelerate and retardate". His view on the oscillation and "alternately accelerated and retardated" motion of the Earth's rotation is a "dynamic process" that deviated from the previous dogma, which proposed "a process of expansion and contraction of seawater." However, Galileo's theory was erroneous. In subsequent centuries, further analysis led to the current tidal physics. Galileo tried to use his tidal theory to prove the movement of the Earth around the Sun. Galileo theorized that because of the Earth's motion, borders of the oceans like the Atlantic and Pacific would show one high tide and one low tide per day. The Mediterranean Sea had two high tides and low tides, though Galileo argued that this was a product of secondary effects and that his theory would hold in the Atlantic. However, Galileo's contemporaries noted that the Atlantic also had two high tides and low tides per day, which led to Galileo omitting this claim from his 1632 Dialogue.

René Descartes theorized that the tides (alongside the movement of planets, etc.) were caused by aetheric vortices, without reference to Kepler's theories of gravitation by mutual attraction; this was extremely influential, with numerous followers of Descartes expounding on this theory throughout the 17th century, particularly in France. However, Descartes and his followers acknowledged the influence of the Moon, speculating that pressure waves from the Moon via the aether were responsible for the correlation.

Newton's three-body model

Newton, in the Principia, provides a correct explanation for the tidal force, which can be used to explain tides on a planet covered by a uniform ocean but which takes no account of the distribution of the continents or ocean bathymetry.

Dynamic theory

While Newton explained the tides by describing the tide-generating forces and Daniel Bernoulli gave a description of the static reaction of the waters on Earth to the tidal potential, the dynamic theory of tides, developed by Pierre-Simon Laplace in 1775, describes the ocean's real reaction to tidal forces. Laplace's theory of ocean tides takes into account friction, resonance and natural periods of ocean basins. It predicts the large amphidromic systems in the world's ocean basins and explains the oceanic tides that are actually observed.

The equilibrium theory—based on the gravitational gradient from the Sun and Moon but ignoring the Earth's rotation, the effects of continents, and other important effects—could not explain the real ocean tides. Since measurements have confirmed the dynamic theory, many things have possible explanations now, like how the tides interact with deep sea ridges, and chains of seamounts give rise to deep eddies that transport nutrients from the deep to the surface. The equilibrium tide theory calculates the height of the tide wave of less than half a meter, while the dynamic theory explains why tides are up to 15 meters.

Satellite observations confirm the accuracy of the dynamic theory, and the tides worldwide are now measured to within a few centimeters. Measurements from the CHAMP satellite closely match the models based on the TOPEX data. Accurate models of tides worldwide are essential for research since the variations due to tides must be removed from measurements when calculating gravity and changes in sea levels.

Laplace's tidal equations

A. Lunar gravitational potential: this depicts the Moon directly over 30° N (or 30° S) viewed from above the Northern Hemisphere. Note however that the moon is never more than about 28.6° north of the equator.

B. This view shows same potential from 180° from view A. Viewed from above the Northern Hemisphere. Red up, blue down.

In 1776, Laplace formulated a single set of linear partial differential equations for tidal flow described as a barotropic two-dimensional sheet flow. Coriolis effects are introduced as well as lateral forcing by gravity. Laplace obtained these equations by simplifying the fluid dynamics equations, but they can also be derived from energy integrals via Lagrange's equation.

For a fluid sheet of average thickness D, the vertical tidal elevation ζ, as well as the horizontal velocity components u and v (in the latitude φ and longitude λ directions, respectively) satisfy Laplace's tidal equations:

${\begin{aligned}{\frac {\partial \zeta }{\partial t}}&+{\frac {1}{a\cos(\varphi )}}\left[{\frac {\partial }{\partial \lambda }}(uD)+{\frac {\partial }{\partial \varphi }}\left(vD\cos(\varphi )\right)\right]=0,\\[2ex]{\frac {\partial u}{\partial t}}&-v\,2\Omega \sin(\varphi )+{\frac {1}{a\cos(\varphi )}}{\frac {\partial }{\partial \lambda }}\left(g\zeta +U\right)=0,\quad {\text{and}}\\[2ex]{\frac {\partial v}{\partial t}}&+u\,2\Omega \sin(\varphi )+{\frac {1}{a}}{\frac {\partial }{\partial \varphi }}\left(g\zeta +U\right)=0,\end{aligned}}$

where Ω is the angular frequency of the planet's rotation, g is the planet's gravitational acceleration at the mean ocean surface, a is the planetary radius, and U is the external gravitational tidal-forcing potential.

William Thomson (Lord Kelvin) rewrote Laplace's momentum terms using the curl to find an equation for vorticity. Under certain conditions this can be further rewritten as a conservation of vorticity.

Tidal analysis and prediction

Harmonic analysis

Spectrum of tides measured at Ft. Pulaski in 2012. Data downloaded from http://tidesandcurrents.noaa.gov/datums.html?id=8670870 Fourier transform computed with https://sourceforge.net/projects/amoreaccuratefouriertransform/

Laplace's improvements in theory were substantial, but they still left prediction in an approximate state. This position changed in the 1860s when the local circumstances of tidal phenomena were more fully brought into account by William Thomson's application of Fourier analysis to the tidal motions as harmonic analysis. Thomson's work in this field was further developed and extended by George Darwin, applying the lunar theory current in his time. Darwin's symbols for the tidal harmonic constituents are still used, for example: M: moon/lunar; S: sun/solar; K: moon-sun/lunisolar.

Darwin's harmonic developments of the tide-generating forces were later improved when A.T. Doodson, applying the lunar theory of E.W. Brown, developed the tide-generating potential (TGP) in harmonic form, distinguishing 388 tidal frequencies. Doodson's work was carried out and published in 1921. Doodson devised a practical system for specifying the different harmonic components of the tide-generating potential, the Doodson numbers, a system still in use.

Since the mid-twentieth century further analysis has generated many more terms than Doodson's 388. About 62 constituents are of sufficient size to be considered for possible use in marine tide prediction, but sometimes many fewer can predict tides to useful accuracy. The calculations of tide predictions using the harmonic constituents are laborious, and from the 1870s to about the 1960s they were carried out using a mechanical tide-predicting machine, a special-purpose form of analog computer. More recently digital computers, using the method of matrix inversion, are used to determine the tidal harmonic constituents directly from tide gauge records.

Tidal constituents

Further information: Tide § Constituents

Tidal prediction summing constituent parts.

Tidal constituents combine to give an endlessly varying aggregate because of their different and incommensurable frequencies: the effect is visualized in an animation of the American Mathematical Society illustrating the way in which the components used to be mechanically combined in the tide-predicting machine. Amplitudes (half of peak-to-peak amplitude) of tidal constituents are given below for six example locations: Eastport, Maine (ME), Biloxi, Mississippi (MS), San Juan, Puerto Rico (PR), Kodiak, Alaska (AK), San Francisco, California (CA), and Hilo, Hawaii (HI).

Semi-diurnal

Species	Darwin symbol	Period (h)	Speed (°/h)	Doodson coefficients				Doodson number	Amplitude at example location (cm)						NOAA order
				n1 (L)	n2 (m)	n3 (y)	n4 (mp)		ME	MS	PR	AK	CA	HI
Principal lunar semidiurnal	M2	12.4206012	28.9841042	2				255.555	268.7	3.9	15.9	97.3	58.0	23.0	1
Principal solar semidiurnal	S2	12	30	2	2	−2		273.555	42.0	3.3	2.1	32.5	13.7	9.2	2
Larger lunar elliptic semidiurnal	N2	12.65834751	28.4397295	2	−1		1	245.655	54.3	1.1	3.7	20.1	12.3	4.4	3
Larger lunar evectional	ν2	12.62600509	28.5125831	2	−1	2	−1	247.455	12.6	0.2	0.8	3.9	2.6	0.9	11
Variational	μ2	12.8717576	27.9682084	2	−2	2		237.555	2.0	0.1	0.5	2.2	0.7	0.8	13
Lunar elliptical semidiurnal second-order	2N2	12.90537297	27.8953548	2	−2		2	235.755	6.5	0.1	0.5	2.4	1.4	0.6	14
Smaller lunar evectional	λ2	12.22177348	29.4556253	2	1	−2	1	263.655	5.3		0.1	0.7	0.6	0.2	16
Larger solar elliptic	T2	12.01644934	29.9589333	2	2	−3		272.555	3.7	0.2	0.1	1.9	0.9	0.6	27
Smaller solar elliptic	R2	11.98359564	30.0410667	2	2	−1		274.555	0.9			0.2	0.1	0.1	28
Shallow water semidiurnal	2SM2	11.60695157	31.0158958	2	4	−4		291.555	0.5						31
Smaller lunar elliptic semidiurnal	L2	12.19162085	29.5284789	2	1		−1	265.455	13.5	0.1	0.5	2.4	1.6	0.5	33
Lunisolar semidiurnal	K2	11.96723606	30.0821373	2	2			275.555	11.6	0.9	0.6	9.0	4.0	2.8	35

Diurnal

Species	Darwin symbol	Period (h)	Speed (°/h)	Doodson coefficients				Doodson number	Amplitude at example location (cm)						NOAA order
				n1 (L)	n2 (m)	n3 (y)	n4 (mp)		ME	MS	PR	AK	CA	HI
Lunisolar diurnal	K1	23.93447213	15.0410686	1	1			165.555	15.6	16.2	9.0	39.8	36.8	16.7	4
Lunar diurnal	O1	25.81933871	13.9430356	1	−1			145.555	11.9	16.9	7.7	25.9	23.0	9.2	6
Lunar diurnal	OO1	22.30608083	16.1391017	1	3			185.555	0.5	0.7	0.4	1.2	1.1	0.7	15
Solar diurnal	S1	24	15	1	1	−1		164.555	1.0		0.5	1.2	0.7	0.3	17
Smaller lunar elliptic diurnal	M1	24.84120241	14.4920521	1				155.555	0.6	1.2	0.5	1.4	1.1	0.5	18
Smaller lunar elliptic diurnal	J1	23.09848146	15.5854433	1	2		−1	175.455	0.9	1.3	0.6	2.3	1.9	1.1	19
Larger lunar evectional diurnal	ρ	26.72305326	13.4715145	1	−2	2	−1	137.455	0.3	0.6	0.3	0.9	0.9	0.3	25
Larger lunar elliptic diurnal	Q1	26.868350	13.3986609	1	−2		1	135.655	2.0	3.3	1.4	4.7	4.0	1.6	26
Larger elliptic diurnal	2Q1	28.00621204	12.8542862	1	−3		2	125.755	0.3	0.4	0.2	0.7	0.4	0.2	29
Solar diurnal	P1	24.06588766	14.9589314	1	1	−2		163.555	5.2	5.4	2.9	12.6	11.6	5.1	30

Long period

Species	Darwin symbol	Period (h) (days)	Speed (°/h)	Doodson coefficients				Doodson number	Amplitude at example location (cm)						NOAA order
				n1 (L)	n2 (m)	n3 (y)	n4 (mp)		ME	MS	PR	AK	CA	HI
Lunar monthly	Mm	661.3111655 27.554631896	0.5443747	0	1		−1	65.455			0.7	1.9			20
Solar semiannual	Ssa	4383.076325 182.628180208	0.0821373	0		2		57.555	1.6		2.1	1.5	3.9		21
Solar annual	Sa	8766.15265 365.256360417	0.0410686	0		1		56.555			5.5	7.8	3.8	4.3	22
Lunisolar synodic fortnightly	MSf	354.3670666 14.765294442	1.0158958	0	2	−2		73.555				1.5			23
Lunisolar fortnightly	Mf	327.8599387 13.660830779	1.0980331	0	2			75.555			1.4	2.0		0.7	24

Short period

Species	Darwin symbol	Period (h)	Speed (°/h)	Doodson coefficients				Doodson number	Amplitude at example location (cm)						NOAA order
				n1 (L)	n2 (m)	n3 (y)	n4 (mp)		ME	MS	PR	AK	CA	HI
Shallow water overtides of principal lunar	M4	6.210300601	57.9682084	4				455.555	6.0	0.6		0.9	2.3		5
Shallow water overtides of principal lunar	M6	4.140200401	86.9523127	6				655.555	5.1	0.1		1.0			7
Shallow water terdiurnal	MK3	8.177140247	44.0251729	3	1			365.555				0.5	1.9		8
Shallow water overtides of principal solar	S4	6	60	4	4	−4		491.555		0.1					9
Shallow water quarter diurnal	MN4	6.269173724	57.4238337	4	−1		1	445.655	2.3			0.3	0.9		10
Shallow water overtides of principal solar	S6	4	90	6	6	−6		*		0.1					12
Lunar terdiurnal	M3	8.280400802	43.4761563	3				355.555					0.5		32
Shallow water terdiurnal	2MK3	8.38630265	42.9271398	3	−1			345.555	0.5			0.5	1.4		34
Shallow water eighth diurnal	M8	3.105150301	115.9364166	8				855.555	0.5	0.1					36
Shallow water quarter diurnal	MS4	6.103339275	58.9841042	4	2	−2		473.555	1.8			0.6	1.0		37

Doodson numbers

In order to specify the different harmonic components of the tide-generating potential, Doodson devised a practical system which is still in use, involving what are called the Doodson numbers based on the six Doodson arguments or Doodson variables. The number of different tidal frequency components is large, but each corresponds to a specific linear combination of six frequencies using small-integer multiples, positive or negative. In principle, these basic angular arguments can be specified in numerous ways; Doodson's choice of his six "Doodson arguments" has been widely used in tidal work. In terms of these Doodson arguments, each tidal frequency can then be specified as a sum made up of a small integer multiple of each of the six arguments. The resulting six small integer multipliers effectively encode the frequency of the tidal argument concerned, and these are the Doodson numbers: in practice all except the first are usually biased upwards by +5 to avoid negative numbers in the notation. (In the case that the biased multiple exceeds 9, the system adopts X for 10, and E for 11.)

The Doodson arguments are specified in the following way, in order of decreasing frequency:

$\beta _{1}=\tau =(\theta _{M}+\pi -s)$ is mean Lunar time, the Greenwich hour angle of the mean Moon plus 12 hours.

$\beta _{2}=s=(F+\Omega )$ is the mean longitude of the Moon.

$\beta _{3}=h=(s-D)$ is the mean longitude of the Sun.

$\beta _{4}=p=(s-l)$ is the longitude of the Moon's mean perigee.

$\beta _{5}=N'=(-\Omega )$ is the negative of the longitude of the Moon's mean ascending node on the ecliptic.

$\beta _{6}=p_{l}$ or $p_{s}=(s-D-l')$ is the longitude of the Sun's mean perigee.

In these expressions, the symbols $l$, $l'$, $F$ and $D$ refer to an alternative set of fundamental angular arguments (usually preferred for use in modern lunar theory), in which:-

$l$ is the mean anomaly of the Moon (distance from its perigee).

$l'$ is the mean anomaly of the Sun (distance from its perigee).

$F$ is the Moon's mean argument of latitude (distance from its node).

$D$ is the Moon's mean elongation (distance from the sun).

It is possible to define several auxiliary variables on the basis of combinations of these.

In terms of this system, each tidal constituent frequency can be identified by its Doodson numbers. The strongest tidal constituent "M₂" has a frequency of 2 cycles per lunar day, its Doodson numbers are usually written 255.555, meaning that its frequency is composed of twice the first Doodson argument, and zero times all of the others. The second strongest tidal constituent "S₂" is influenced by the sun, and its Doodson numbers are 273.555, meaning that its frequency is composed of twice the first Doodson argument, +2 times the second, -2 times the third, and zero times each of the other three. This aggregates to the angular equivalent of mean solar time +12 hours. These two strongest component frequencies have simple arguments for which the Doodson system might appear needlessly complex, but each of the hundreds of other component frequencies can be briefly specified in a similar way, showing in the aggregate the usefulness of the encoding.

See also

• Long-period tides
• Lunar node § Effect on tides
• Kelvin wave
• Tide table

External links

• Contributions of satellite laser ranging to the studies of earth tides Archived 28 July 2013 at the Wayback Machine
• Dynamic Theory of Tides
• Tidal Observations
• Publications from NOAA's Center for Operational Oceanographic Products and Services
  • Understanding Tides
  • 150 Years of Tides on the Western Coast
  • Our Relentless Tides
  • GeoTide Tidal Analysis System