High tide, Alma, New Brunswick in the Bay of Fundy		Low tide at the same fishing port in Bay of Fundy

Tides (from low-German 'tiet' = 'time') are the rise and fall of sea levels caused by the combined effects of the gravitational forces exerted by the Moon and the Sun and the rotation of the Earth.

Most places in the ocean usually experience two high tides and two low tides each day (semi-diurnal tide), but some locations experience only one high and one low tide each day (diurnal tide). The times and amplitude of the tides at the coast are influenced by the alignment of the Sun and Moon, by the pattern of tides in the deep ocean and by the shape of the coastline and near-shore bathymetry (see Timing).^[1][2][3]

Tides vary on timescales ranging from hours to years due to numerous influences. To make accurate records, tide gauges at fixed stations measure the water level over time. Gauges ignore variations caused by waves with periods shorter than minutes. These data are compared to the reference (or datum) level usually called mean sea level.^[4]

While tides are usually the largest source of short-term sea-level fluctuations, sea levels are also subject to forces such as wind and barometric pressure changes, resulting in storm surges, especially in shallow seas and near coasts.

Tidal phenomena are not limited to the oceans, but can occur in other systems whenever a gravitational field that varies in time and space is present. For example, the solid part of the Earth is affected by tides, though this is not as easily seen as the water tidal movements.

Characteristics[link]

Tide changes proceed via the following stages:

• Sea level rises over several hours, covering the intertidal zone; flood tide.
• The water rises to its highest level, reaching high tide.
• Sea level falls over several hours, revealing the intertidal zone; ebb tide.
• The water stops falling, reaching low tide.

Tides produce oscillating currents known as tidal streams. The moment that the tidal current ceases is called slack water or slack tide. The tide then reverses direction and is said to be turning. Slack water usually occurs near high water and low water. But there are locations where the moments of slack tide differ significantly from those of high and low water.^[5]

Tides are most commonly semi-diurnal (two high waters and two low waters each day), or diurnal (one tidal cycle per day). The two high waters on a given day are typically not the same height (the daily inequality); these are the higher high water and the lower high water in tide tables. Similarly, the two low waters each day are the higher low water and the lower low water. The daily inequality is not consistent and is generally small when the Moon is over the equator.^[6]

Tidal constituents[link]

Tidal changes are the net result of multiple influences that act over varying periods. These influences are called tidal constituents. The primary constituents are the Earth's rotation, the positions of the Moon and the Sun relative to Earth, the Moon's altitude (elevation) above the Earth's equator, and bathymetry.

Variations with periods of less than half a day are called harmonic constituents. Conversely, cycles of days, months, or years are referred to as long period constituents.

The tidal forces affect the entire earth, but the movement of the solid Earth is only centimeters. The atmosphere is much more fluid and compressible so its surface moves kilometers, in the sense of the contour level of a particular low pressure in the outer atmosphere.

Principal lunar semi-diurnal constituent[link]

In most locations, the largest constituent is the "principal lunar semi-diurnal", also known as the M2 (or M₂) tidal constituent. Its period is about 12 hours and 25.2 minutes, exactly half a tidal lunar day, which is the average time separating one lunar zenith from the next, and thus is the time required for the Earth to rotate once relative to the Moon. Simple tide clocks track this constituent. The lunar day is longer than the Earth day because the Moon orbits in the same direction the Earth spins. This is analogous to the minute hand on a watch crossing the hour hand at 12:00 and then again at about 1:05½ (not at 1:00).

The Moon orbits the Earth in the same direction as the Earth rotates on its axis, so it takes slightly more than a day—about 24 hours and 50 minutes—for the Moon to return to the same location in the sky. During this time, it has passed overhead (culmination) once and underfoot once (at an hour angle of 00:00 and 12:00 respectively), so in many places the period of strongest tidal forcing is the above mentioned, about 12 hours and 25 minutes. The moment of highest tide is not necessarily when the Moon is nearest to zenith or nadir, but the period of the forcing still determines the time between high tides.

Because the gravitational field created by the Moon weakens with distance from the Moon, it exerts a slightly stronger force on the side of the Earth facing the Moon than average, and a slightly weaker force on the opposite side. The Moon thus tends to "stretch" the Earth slightly along the line connecting the two bodies. The solid Earth deforms a bit, but ocean water, being fluid, is free to move much more in response to the tidal force, particularly horizontally. As the Earth rotates, the magnitude and direction of the tidal force at any particular point on the Earth's surface change constantly; although the ocean never reaches equilibrium—there is never time for the fluid to "catch up" to the state it would eventually reach if the tidal force were constant—the changing tidal force nonetheless causes rhythmic changes in sea surface height.

Semi-diurnal range differences[link]

When there are two high tides each day with different heights (and two low tides also of different heights), the pattern is called a mixed semi-diurnal tide.^[7]

Range variation: springs and neaps[link]

The types of tides

The semi-diurnal range (the difference in height between high and low waters over about half a day) varies in a two-week cycle. Approximately twice a month, around new moon and full moon when the Sun, Moon and Earth form a line (a condition known as syzygy^[8]) the tidal force due to the sun reinforces that due to the Moon. The tide's range is then at its maximum: this is called the spring tide, or just springs. It is not named after the season but, like that word, derives from the meaning "jump, burst forth, rise", as in a natural spring.

When the Moon is at first quarter or third quarter, the sun and Moon are separated by 90° when viewed from the Earth, and the solar tidal force partially cancels the Moon's. At these points in the lunar cycle, the tide's range is at its minimum: this is called the neap tide, or neaps (a word of uncertain origin).

Spring tides result in high waters that are higher than average, low waters that are lower than average, 'slack water' time that is shorter than average and stronger tidal currents than average. Neaps result in less extreme tidal conditions. There is about a seven-day interval between springs and neaps.

Lunar altitude[link]

Negative low tide at Ocean Beach in San Francisco

The changing distance separating the Moon and Earth also affects tide heights. When the Moon is closest, at perigee, the range increases, and when it is at apogee, the range shrinks. Every 7½ lunations (the full cycles from full moon to new to full), perigee coincides with either a new or full moon causing perigean spring tides with the largest tidal range. Even at its most powerful this force is still weak^[9] causing tidal differences of inches at most.^[10]

Bathymetry[link]

The shape of the shoreline and the ocean floor changes the way that tides propagate, so there is no simple, general rule that predicts the time of high water from the Moon's position in the sky. Coastal characteristics such as underwater bathymetry and coastline shape mean that individual location characteristics affect tide forecasting; actual high water time and height may differ from model predictions due to the coastal morphology's effects on tidal flow. However, for a given location the relationship between lunar altitude and the time of high or low tide (the lunitidal interval) is relatively constant and predictable, as is the time of high or low tide relative to other points on the same coast. For example, the high tide at Norfolk, Virginia, predictably occurs approximately two and a half hours before the Moon passes directly overhead.

Land masses and ocean basins act as barriers against water moving freely around the globe, and their varied shapes and sizes affect the size of tidal frequencies. As a result, tidal patterns vary. For example, in the U.S., the East coast has predominantly semi-diurnal tides, as do Europe's Atlantic coasts, while the West coast predominantly has mixed tides.^[11][12][13]

Other constituents[link]

These include solar gravitational effects, the obliquity (tilt) of the Earth's equator and rotational axis, the inclination of the plane of the lunar orbit and the elliptical shape of the Earth's orbit of the sun.

A compound tide (or overtide) results from the shallow-water interaction of its two parent waves.^[14]

Phase and amplitude[link]

The M₂ tidal constituent. Amplitude is indicated by color, and the white lines are cotidal differing by 1 hour. The curved arcs around the amphidromic points show the direction of the tides, each indicating a synchronized 6-hour period.^[15][16]

Because the M₂ tidal constituent dominates in most locations, the stage or phase of a tide, denoted by the time in hours after high water, is a useful concept. Tidal stage is also measured in degrees, with 360° per tidal cycle. Lines of constant tidal phase are called cotidal lines, which are analogous to contour lines of constant altitude on topographical maps. High water is reached simultaneously along the cotidal lines extending from the coast out into the ocean, and cotidal lines (and hence tidal phases) advance along the coast. Semi-diurnal and long phase constituents are measured from high water, diurnal from maximum flood tide. This and the discussion that follows is precisely true only for a single tidal constituent.

For an ocean in the shape of a circular basin enclosed by a coastline, the cotidal lines point radially inward and must eventually meet at a common point, the amphidromic point. The amphidromic point is at once cotidal with high and low waters, which is satisfied by zero tidal motion. (The rare exception occurs when the tide encircles an island, as it does around New Zealand, Iceland and Madagascar.) Tidal motion generally lessens moving away from continental coasts, so that crossing the cotidal lines are contours of constant amplitude (half the distance between high and low water) which decrease to zero at the amphidromic point. For a semi-diurnal tide the amphidromic point can be thought of roughly like the center of a clock face, with the hour hand pointing in the direction of the high water cotidal line, which is directly opposite the low water cotidal line. High water rotates about the amphidromic point once every 12 hours in the direction of rising cotidal lines, and away from ebbing cotidal lines. This rotation is generally clockwise in the southern hemisphere and counterclockwise in the northern hemisphere, and is caused by the Coriolis effect. The difference of cotidal phase from the phase of a reference tide is the epoch. The reference tide is the hypothetical constituent equilibrium tide on a landless Earth measured at 0° longitude, the Greenwich meridian.

In the North Atlantic, because the cotidal lines circulate counterclockwise around the amphidromic point, the high tide passes New York Harbor approximately an hour ahead of Norfolk Harbor. South of Cape Hatteras the tidal forces are more complex, and cannot be predicted reliably based on the North Atlantic cotidal lines.

Physics[link]

History of tidal physics[link]

Tidal physics was important in the early development of heliocentrism^{[citation needed]} and celestial mechanics, with the existence of two daily tides being explained by the Moon's gravity. Later the daily tides were explained more precisely by the interaction of the Moon's gravity and the sun's gravity to cause the variation of tides.

An early explanation of tides was given by Galileo Galilei in his 1632 Dialogue Concerning the Two Chief World Systems, whose working title was Dialogue on the Tides. However, the resulting theory was incorrect – he attributed the tides to water sloshing due to the Earth's movement around the sun, hoping to provide mechanical proof of the Earth's movement – and the value of the theory is disputed, as discussed there. At the same time Johannes Kepler correctly suggested that the Moon caused the tides, based upon ancient observation and correlations, an explanation which was rejected by Galileo. It was originally mentioned in Ptolemy's Tetrabiblos as being derived from ancient observation.

Isaac Newton (1642–1727) was the first person to explain tides by the gravitational attraction of masses. His explanation of the tides (and many other phenomena) was published in the Principia (1687).^[17][18] and used his theory of universal gravitation to account for the tide-generating forces as due to the lunar and solar attractions.^[19] Newton and others before Pierre-Simon Laplace worked with an equilibrium theory, largely concerned with an approximation that describes the tides that would occur in a non-inertial ocean evenly covering the whole Earth.^[17] The tide-generating force (or its corresponding potential) is still relevant to tidal theory, but as an intermediate quantity rather than as a final result; theory has to consider also the Earth's accumulated dynamic tidal response to the force, a response that is influenced by bathymetry, Earth's rotation, and other factors.^[20]

In 1740, the Académie Royale des Sciences in Paris offered a prize for the best theoretical essay on tides. Daniel Bernoulli, Leonhard Euler, Colin Maclaurin and Antoine Cavalleri shared the prize.

Maclaurin used Newton’s theory to show that a smooth sphere covered by a sufficiently deep ocean under the tidal force of a single deforming body is a prolate spheroid (essentially a three dimensional oval) with major axis directed toward the deforming body. Maclaurin was the first to write about the Earth's rotational effects on motion. Euler realized that the tidal force's horizontal component (more than the vertical) drives the tide. In 1744 Jean le Rond d'Alembert studied tidal equations for the atmosphere which did not include rotation.

Pierre-Simon Laplace formulated a system of partial differential equations relating the ocean's horizontal flow to its surface height, the first major dynamic theory for water tides. The Laplace tidal equations are still in use today. William Thomson, 1st Baron Kelvin, rewrote Laplace's equations in terms of vorticity which allowed for solutions describing tidally driven coastally trapped waves, known as Kelvin waves.^[21][22][23]

Others including Kelvin and Henri Poincaré further developed Laplace's theory. Based on these developments and the lunar theory of E W Brown describing the motions of the Moon, Arthur Thomas Doodson developed and published in 1921^[24] the first modern development of the tide-generating potential in harmonic form: Doodson distinguished 388 tidal frequencies.^[25] Some of his methods remain in use.^[26]

Forces[link]

The tidal force produced by a massive object (Moon, hereafter) on a small particle located on or in an extensive body (Earth, hereafter) is the vector difference between the gravitational force exerted by the Moon on the particle, and the gravitational force that would be exerted on the particle if it were located at the Earth's center of mass. Thus, the tidal force depends not on the strength of the lunar gravitational field, but on its gradient (which falls off approximately as the inverse cube of the distance to the originating gravitational body).^[27][28] The solar gravitational force on the Earth is on average 179 times stronger than the lunar, but because the sun is on average 389 times farther from the Earth, its field gradient is weaker. The solar tidal force is 46% as large as the lunar.^[29] More precisely, the lunar tidal acceleration (along the moon-Earth axis, at the Earth's surface) is about 1.1 × 10⁻⁷ g, while the solar tidal acceleration (along the sun-Earth axis, at the Earth's surface) is about 0.52 × 10⁻⁷ g, where g is the gravitational acceleration at the Earth's surface.^[30] Venus has the largest effect of the other planets, at 0.000113 times the solar effect.

The lunar gravity differential field at the Earth's surface is known as the tide-generating force. This is the primary mechanism that drives tidal action and explains two equipotential tidal bulges, accounting for two daily high waters.

Tidal forces can also be analysed this way: each point of the Earth experiences the moon's radially decreasing gravity differently. Only the tidal forces' horizontal components actually tidally accelerate the water particles since there is small resistance. The tidal force on a particle equals about one ten millionth that of Earth's gravitational force.

The ocean's surface is closely approximated by an equipotential surface, (ignoring ocean currents) commonly referred to as the geoid. Since the gravitational force is equal to the potential's gradient, there are no tangential forces on such a surface, and the ocean surface is thus in gravitational equilibrium. Now consider the effect of massive external bodies such as the moon and sun. These bodies have strong gravitational fields that diminish with distance in space and which act to alter the shape of an equipotential surface on the Earth. This deformation has a fixed spatial orientation relative to the influencing body. The Earth's rotation relative to this shape causes the daily tidal cycle. Gravitational forces follow an inverse-square law (force is inversely proportional to the square of the distance), but tidal forces are inversely proportional to the cube of the distance. The ocean surface moves to adjust to changing tidal equipotential, tending to rise when the tidal potential is high, which occurs on the part of the Earth nearest to and furthest from the moon. When the tidal equipotential changes, the ocean surface is no longer aligned with it, so that the apparent direction of the vertical shifts. The surface then experiences a down slope, in the direction that the equipotential has risen.

Laplace's tidal equations[link]

Ocean depths are much smaller than their horizontal extent. Thus, the response to tidal forcing can be modelled using the Laplace tidal equations which incorporate the following features:

1. The vertical (or radial) velocity is negligible, and there is no vertical shear—this is a sheet flow.
2. The forcing is only horizontal (tangential).
3. The Coriolis effect appears as a fictitious lateral forcing proportional to velocity.
4. The surface height's rate of change is proportional to the negative divergence of velocity multiplied by the depth. As the horizontal velocity stretches or compresses the ocean as a sheet, the volume thins or thickens, respectively.

The boundary conditions dictate no flow across the coastline and free slip at the bottom.

The Coriolis effect steers waves to the right in the northern hemisphere and to the left in the southern allowing coastally trapped waves. Finally, a dissipation term can be added which is an analog to viscosity.^[31]

Amplitude and cycle time[link]

The theoretical amplitude of oceanic tides caused by the moon is about 54 centimetres (21 in) at the highest point, which corresponds to the amplitude that would be reached if the ocean possessed a uniform depth, there were no landmasses, and the Earth were rotating in step with the moon's orbit. The sun similarly causes tides, of which the theoretical amplitude is about 25 centimetres (9.8 in) (46% of that of the moon) with a cycle time of 12 hours. At spring tide the two effects add to each other to a theoretical level of 79 centimetres (31 in), while at neap tide the theoretical level is reduced to 29 centimetres (11 in). Since the orbits of the Earth about the sun, and the moon about the Earth, are elliptical, tidal amplitudes change somewhat as a result of the varying Earth–sun and Earth–moon distances. This causes a variation in the tidal force and theoretical amplitude of about ±18% for the moon and ±5% for the sun. If both the sun and moon were at their closest positions and aligned at new moon, the theoretical amplitude would reach 93 centimetres (37 in).

Real amplitudes differ considerably, not only because of depth variations and continental obstacles, but also because wave propagation across the ocean has a natural period of the same order of magnitude as the rotation period: if there were no land masses, it would take about 30 hours for a long wavelength surface wave to propagate along the equator halfway around the Earth (by comparison, the Earth's lithosphere has a natural period of about 57 minutes). Earth tides, which raise and lower the bottom of the ocean, and the tide's own gravitational self attraction are both significant and further complicate the ocean's response to tidal forces.

Dissipation[link]

Earth's tidal oscillations introduce dissipation at an average rate of about 3.75 terawatt.^[32] About 98% of this dissipation is by marine tidal movement.^[33] Dissipation arises as basin-scale tidal flows drive smaller-scale flows which experience turbulent dissipation. This tidal drag creates torque on the moon that gradually transfers angular momentum to its orbit, and a gradual increase in Earth–moon separation. The equal and opposite torque on the Earth correspondingly decreases its rotational velocity. Thus, over geologic time, the moon recedes from the Earth, at about 3.8 centimetres (1.5 in)/year, lengthening the terrestrial day.^[34] Day length has increased by about 2 hours in the last 600 million years. Assuming (as a crude approximation) that the deceleration rate has been constant, this would imply that 70 million years ago, day length was on the order of 1% shorter with about 4 more days per year.

Observation and prediction[link]

History[link]

Brouscon's Almanach of 1546: Compass bearings of high waters in the Bay of Biscay (left) and the coast from Brittany to Dover (right).

Brouscon's Almanach of 1546: Tidal diagrams "according to the age of the moon".

From ancient times, tidal observation and discussion has increased in sophistication, first marking the daily recurrence, then tides' relationship to the sun and moon. Pytheas travelled to the British Isles about 325 BC and seems to be the first to have related spring tides to the phase of the moon.

In the 2nd century BC, the Babylonian astronomer, Seleucus of Seleucia, correctly described the phenomenon of tides in order to support his heliocentric theory.^[35] He correctly theorized that tides were caused by the moon, although he believed that the interaction was mediated by the pneuma. He noted that tides varied in time and strength in different parts of the world. According to Strabo (1.1.9), Seleucus was the first to link tides to the lunar attraction, and that the height of the tides depends on the moon's position relative to the sun.^[36]

In China, Wang Chong (27–100 AD) correlated tide to the moon's movement in the book entitled Lunheng. He noted that "tide's rise and fall follow the moon and vary in magnitude."^[37]

The Naturalis Historia of Pliny the Elder collates many tidal observations, e.g., the spring tides are a few days after (or before) new and full moon and are highest around the equinoxes, though Pliny noted many relationships now regarded as fanciful. In his Geography, Strabo described tides in the Persian Gulf having their greatest range when the moon was furthest from the plane of the equator. All this despite the relatively small amplitude of Mediterranean basin tides. (The strong currents through the Euripus Strait and the Strait of Messina puzzled Aristotle.) Philostratus discussed tides in Book Five of The Life of Apollonius of Tyana. Philostratus mentions the moon, but attributes tides to "spirits". In Europe around 730 AD, the Venerable Bede described how the rising tide on one coast of the British Isles coincided with the fall on the other and described the time progression of high water along the Northumbrian coast.

In the 9th century, the Arabian earth-scientist, Al-Kindi (Alkindus), wrote a treatise entitled Risala fi l-Illa al-Failali l-Madd wa l-Fazr (Treatise on the Efficient Cause of the Flow and Ebb), in which he presents an argument on tides which "depends on the changes which take place in bodies owing to the rise and fall of temperature."^{[citation needed]} He describes a precise laboratory experiment that proved his argument.^[38]

The first tide table in China was recorded in 1056 AD primarily for visitors wishing to see the famous tidal bore in the Qiantang River. The first known British tide table is thought to be that of John Wallingford, who died Abbot of St. Albans in 1213, based on high water occurring 48 minutes later each day, and three hours earlier at the Thames mouth than upriver at London.

William Thomson (Lord Kelvin) led the first systematic harmonic analysis of tidal records starting in 1867. The main result was the building of a tide-predicting machine using a system of pulleys to add together six harmonic time functions. It was "programmed" by resetting gears and chains to adjust phasing and amplitudes. Similar machines were used until the 1960s.^[39]

The first known sea-level record of an entire spring–neap cycle was made in 1831 on the Navy Dock in the Thames Estuary. Many large ports had automatic tide gage stations by 1850.

William Whewell first mapped co-tidal lines ending with a nearly global chart in 1836. In order to make these maps consistent, he hypothesized the existence of amphidromes where co-tidal lines meet in the mid-ocean. These points of no tide were confirmed by measurement in 1840 by Captain Hewett, RN, from careful soundings in the North Sea.^[21]

Timing[link]

The same tidal forcing has different results depending on many factors, including coast orientation, continental shelf margin, water body dimensions.

There is a delay between the phases of the moon and the effect on the tide. Springs and neaps in the North Sea, for example, are two days behind the new/full moon and first/third quarter moon. This is called the tide's age.^[40][41]

The local bathymetry greatly influences the tide's exact time and height at a particular coastal point. There are some extreme cases: the Bay of Fundy, on the east coast of Canada, features the world's largest well-documented tidal ranges, 17 metres (56 ft) because of its shape.^[42] Some experts^[who?] believe Ungava Bay in northern Quebec to have even higher tidal ranges^{[citation needed]}, but it is free of pack ice for only about four months every year, while the Bay of Fundy rarely freezes.

Southampton in the United Kingdom has a double high water caused by the interaction between the region's different tidal harmonics, caused primarily by the east/west orientation of the English Channel and the fact that when it is high water at Dover it is low water at Land's End (some 300 nautical miles distant) and vice versa. This is contrary to the popular belief that the flow of water around the Isle of Wight creates two high waters. The Isle of Wight is important, however, since it is responsible for the 'Young Flood Stand', which describes the pause of the incoming tide about three hours after low water.^[43]

Because the oscillation modes of the Mediterranean Sea and the Baltic Sea do not coincide with any significant astronomical forcing period, the largest tides are close to their narrow connections with the Atlantic Ocean. Extremely small tides also occur for the same reason in the Gulf of Mexico and Sea of Japan. Elsewhere, as along the southern coast of Australia, low tides can be due to the presence of a nearby amphidrome.

Analysis[link]

A regular water level chart

Isaac Newton's theory of gravitation first enabled an explanation of why there were generally two tides a day, not one, and offered hope for detailed understanding. Although it may seem that tides could be predicted via a sufficiently detailed knowledge of the instantaneous astronomical forcings, the actual tide at a given location is determined by astronomical forces accumulated over many days. Precise results require detailed knowledge of the shape of all the ocean basins—their bathymetry and coastline shape.

Current procedure for analysing tides follows the method of harmonic analysis introduced in the 1860s by William Thomson. It is based on the principle that the astronomical theories of the motions of sun and moon determine a large number of component frequencies, and at each frequency there is a component of force tending to produce tidal motion, but that at each place of interest on the Earth, the tides respond at each frequency with an amplitude and phase peculiar to that locality. At each place of interest, the tide heights are therefore measured for a period of time sufficiently long (usually more than a year in the case of a new port not previously studied) to enable the response at each significant tide-generating frequency to be distinguished by analysis, and to extract the tidal constants for a sufficient number of the strongest known components of the astronomical tidal forces to enable practical tide prediction. The tide heights are expected to follow the tidal force, with a constant amplitude and phase delay for each component. Because astronomical frequencies and phases can be calculated with certainty, the tide height at other times can then be predicted once the response to the harmonic components of the astronomical tide-generating forces has been found.

The main patterns in the tides are

• the twice-daily variation
• the difference between the first and second tide of a day
• the spring–neap cycle
• the annual variation

The Highest Astronomical Tide is the perigean spring tide when both the sun and the moon are closest to the Earth.

When confronted by a periodically varying function, the standard approach is to employ Fourier series, a form of analysis that uses sinusoidal functions as a basis set, having frequencies that are zero, one, two, three, etc. times the frequency of a particular fundamental cycle. These multiples are called harmonics of the fundamental frequency, and the process is termed harmonic analysis. If the basis set of sinusoidal functions suit the behaviour being modelled, relatively few harmonic terms need to be added. Orbital paths are very nearly circular, so sinusoidal variations are suitable for tides.

For the analysis of tide heights, the Fourier series approach has in practice to be made more elaborate than the use of a single frequency and its harmonics. The tidal patterns are decomposed into many sinusoids having many fundamental frequencies, corresponding (as in the lunar theory) to many different combinations of the motions of the Earth, the moon, and the angles that define the shape and location of their orbits.

For tides, then, harmonic analysis is not limited to harmonics of a single frequency.^[44] In other words, the harmonies are multiples of many fundamental frequencies, not just of the fundamental frequency of the simpler Fourier series approach. Their representation as a Fourier series having only one fundamental frequency and its (integer) multiples would require many terms, and would be severely limited in the time-range for which it would be valid.

The study of tide height by harmonic analysis was begun by Laplace, William Thomson (Lord Kelvin), and George Darwin. A.T. Doodson extended their work, introducing the Doodson Number notation to organise the hundreds of resulting terms. This approach has been the international standard ever since, and the complications arise as follows: the tide-raising force is notionally given by sums of several terms. Each term is of the form

A·cos(w·t + p)

where A is the amplitude, w is the angular frequency usually given in degrees per hour corresponding to t measured in hours, and p is the phase offset with regard to the astronomical state at time t = 0 . There is one term for the moon and a second term for the sun. The phase p of the first harmonic for the moon term is called the lunitidal interval or high water interval. The next step is to accommodate the harmonic terms due to the elliptical shape of the orbits. Accordingly, the value of A is not a constant but also varying with time, slightly, about some average figure. Replace it then by A(t) where A is another sinusoid, similar to the cycles and epicycles of Ptolemaic theory. Accordingly,

A(t) = A·(1 + A_a·cos(w_a·t + p_a)) ,

which is to say an average value A with a sinusoidal variation about it of magnitude A_a , with frequency w_a and phase p_a . Thus the simple term is now the product of two cosine factors:

A·[1 + A_a·cos(w_a + p_a)]·cos(w·t + p)

Given that for any x and y

cos(x)·cos(y) = ½·cos( x + y ) + ½·cos( x–y ) ,

it is clear that a compound term involving the product of two cosine terms each with their own frequency is the same as three simple cosine terms that are to be added at the original frequency and also at frequencies which are the sum and difference of the two frequencies of the product term. (Three, not two terms, since the whole expression is (1 + cos(x))·cos(y) .) Consider further that the tidal force on a location depends also on whether the moon (or the sun) is above or below the plane of the equator, and that these attributes have their own periods also incommensurable with a day and a month, and it is clear that many combinations result. With a careful choice of the basic astronomical frequencies, the Doodson Number annotates the particular additions and differences to form the frequency of each simple cosine term.

Remember that astronomical tides do not include weather effects. Also, changes to local conditions (sandbank movement, dredging harbour mouths, etc.) away from those prevailing at the measurement time affect the tide's actual timing and magnitude. Organisations quoting a "highest astronomical tide" for some location may exaggerate the figure as a safety factor against analytical uncertainties, distance from the nearest measurement point, changes since the last observation time, ground subsidence, etc., to avert liability should an engineering work be overtopped. Special care is needed when assessing the size of a "weather surge" by subtracting the astronomical tide from the observed tide.

Careful Fourier data analysis over a nineteen-year period (the National Tidal Datum Epoch in the U.S.) uses frequencies called the tidal harmonic constituents. Nineteen years is preferred because the Earth, moon and sun's relative positions repeat almost exactly in the Metonic cycle of 19 years, which is long enough to include the 18.613 year lunar nodal tidal constituent. This analysis can be done using only the knowledge of the forcing period, but without detailed understanding of the mathematical derivation, which means that useful tidal tables have been constructed for centuries.^[45] The resulting amplitudes and phases can then be used to predict the expected tides. These are usually dominated by the constituents near 12 hours (the semi-diurnal constituents), but there are major constituents near 24 hours (diurnal) as well. Longer term constituents are 14 day or fortnightly, monthly, and semiannual. Semi-diurnal tides dominated coastline, but some areas such as the South China Sea and the Gulf of Mexico are primarily diurnal. In the semi-diurnal areas, the primary constituents M₂ (lunar) and S₂ (solar) periods differ slightly, so that the relative phases, and thus the amplitude of the combined tide, change fortnightly (14 day period).^[46]

In the M₂ plot above, each cotidal line differs by one hour from its neighbors, and the thicker lines show tides in phase with equilibrium at Greenwich. The lines rotate around the amphidromic points counterclockwise in the northern hemisphere so that from Baja California Peninsula to Alaska and from France to Ireland the M₂ tide propagates northward. In the southern hemisphere this direction is clockwise. On the other hand M₂ tide propagates counterclockwise around New Zealand, but this is because the islands act as a dam and permit the tides to have different heights on the islands' opposite sides. (The tides do propagate northward on the east side and southward on the west coast, as predicted by theory.)

The exception is at Cook Strait where the tidal currents periodically link high to low water. This is because cotidal lines 180° around the amphidromes are in opposite phase, for example high water across from low water at each end of Cook Strait. Each tidal constituent has a different pattern of amplitudes, phases, and amphidromic points, so the M₂ patterns cannot be used for other tide components.

Example calculation[link]

Because the moon is moving in its orbit around the earth and in the same sense as the Earth's rotation, a point on the earth must rotate slightly further to catch up so that the time between semidiurnal tides is not twelve but 12.4206 hours—a bit over twenty-five minutes extra. The two peaks are not equal. The two high tides a day alternate in maximum heights: lower high (just under three feet), higher high (just over three feet), and again lower high. Likewise for the low tides.

When the Earth, moon, and sun are in line (sun–Earth–moon, or sun–moon–Earth) the two main influences combine to produce spring tides; when the two forces are opposing each other as when the angle moon–Earth–sun is close to ninety degrees, neap tides result. As the moon moves around its orbit it changes from north of the equator to south of the equator. The alternation in high tide heights becomes smaller, until they are the same (at the lunar equinox, the moon is above the equator), then redevelop but with the other polarity, waxing to a maximum difference and then waning again.

Current[link]

The tides' influence on current flow is much more difficult to analyse, and data is much more difficult to collect. A tidal height is a simple number which applies to a wide region simultaneously. A flow has both a magnitude and a direction, both of which can vary substantially with depth and over short distances due to local bathymetry. Also, although a water channel's center is the most useful measuring site, mariners object when current-measuring equipment obstructs waterways. A flow proceeding up a curved channel is the same flow, even though its direction varies continuously along the channel. Surprisingly, flood and ebb flows are often not in opposite directions. Flow direction is determined by the upstream channel's shape, not the downstream channel's shape. Likewise, eddies may form in only one flow direction.

Nevertheless, current analysis is similar to tidal analysis: in the simple case, at a given location the flood flow is in mostly one direction, and the ebb flow in another direction. Flood velocities are given positive sign, and ebb velocities negative sign. Analysis proceeds as though these are tide heights.

In more complex situations, the main ebb and flood flows do not dominate. Instead, the flow direction and magnitude trace an ellipse over a tidal cycle (on a polar plot) instead of along the ebb and flood lines. In this case, analysis might proceed along pairs of directions, with the primary and secondary directions at right angles. An alternative is to treat the tidal flows as complex numbers, as each value has both a magnitude and a direction.

Tide flow information is most commonly seen on nautical charts, presented as a table of flow speeds and bearings at hourly intervals, with separate tables for spring and neap tides. The timing is relative to high water at some harbour where the tidal behaviour is similar in pattern, though it may be far away.

As with tide height predictions, tide flow predictions based only on astronomical factors do not incorporate weather conditions, which can completely change the outcome.

The tidal flow through Cook Strait between the two main islands of New Zealand is particularly interesting, as the tides on each side of the strait are almost exactly out of phase, so that one side's high water is simultaneous with the other's low water. Strong currents result, with almost zero tidal height change in the strait's center. Yet, although the tidal surge normally flows in one direction for six hours and in the reverse direction for six hours, a particular surge might last eight or ten hours with the reverse surge enfeebled. In especially boisterous weather conditions, the reverse surge might be entirely overcome so that the flow continues in the same direction through three or more surge periods.

A further complication for Cook Strait's flow pattern is that the tide at the north side (e.g. at Nelson) follows the common bi-weekly spring–neap tide cycle (as found along the west side of the country), but the south side's tidal pattern has only one cycle per month, as on the east side: Wellington, and Napier.

Figure 12 shows separately the high water and low water height and time, through November 2007; these are not measured values but instead are calculated from tidal parameters derived from years-old measurements. Cook Strait's nautical chart offers tidal current information. For instance the January 1979 edition for 41°13·9’S 174°29·6’E (north west of Cape Terawhiti) refers timings to Westport while the January 2004 issue refers to Wellington. Near Cape Terawhiti in the middle of Cook Strait the tidal height variation is almost nil while the tidal current reaches its maximum, especially near the notorious Karori Rip. Aside from weather effects, the actual currents through Cook Strait are influenced by the tidal height differences between the two ends of the strait and as can be seen, only one of the two spring tides at the north end (Nelson) has a counterpart spring tide at the south end (Wellington), so the resulting behaviour follows neither reference harbour.^{[citation needed]}

Power generation[link]

Tidal energy can be extracted by two means: inserting a water turbine into a tidal current, or building ponds that release/admit water through a turbine. In the first case, the energy amount is entirely determined by the timing and tidal current magnitude. However, the best currents may be unavailable because the turbines would obstruct ships. In the second, the impoundment dams are expensive to construct, natural water cycles are completely disrupted, ship navigation is disrupted. However, with multiple ponds, power can be generated at chosen times. So far, there are few installed systems for tidal power generation (most famously, La Rance by Saint Malo, France) which faces many difficulties. Aside from environmental issues, simply withstanding corrosion and biological fouling pose engineering challenges.

Tidal power proponents point out that, unlike wind power systems, generation levels can be reliably predicted, save for weather effects. While some generation is possible for most of the tidal cycle, in practice turbines lose efficiency at lower operating rates. Since the power available from a flow is proportional to the cube of the flow speed, the times during which high power generation is possible are brief.

Navigation[link]

Tidal flows are important for navigation, and significant errors in position occur if they are not accommodated. Tidal heights are also important; for example many rivers and harbours have a shallow "bar" at the entrance which prevents boats with significant draft from entering at low tide.

Until the advent of automated navigation, competence in calculating tidal effects was important to naval officers. The certificate of examination for lieutenants in the Royal Navy once declared that the prospective officer was able to "shift his tides".^[47]

Tidal flow timings and velocities appear in tide charts or a tidal stream atlas. Tide charts come in sets. Each chart covers a single hour between one high water and another (they ignore the leftover 24 minutes) and show the average tidal flow for that hour. An arrow on the tidal chart indicates the direction and the average flow speed (usually in knots) for spring and neap tides. If a tide chart is not available, most nautical charts have "tidal diamonds" which relate specific points on the chart to a table giving tidal flow direction and speed.

The standard procedure to counteract tidal effects on navigation is to (1) calculate a "dead reckoning" position (or DR) from travel distance and direction, (2) mark the chart (with a vertical cross like a plus sign) and (3) draw a line from the DR in the tide's direction. The distance the tide moves the boat along this line is computed by the tidal speed, and this gives an "estimated position" or EP (traditionally marked with a dot in a triangle).

Nautical charts display the water's "charted depth" at specific locations with "soundings" and the use of bathymetric contour lines to depict the submerged surface's shape. These depths are relative to a "chart datum", which is typically the water level at the lowest possible astronomical tide (although other datums are commonly used, especially historically, and tides may be lower or higher for meteorological reasons) and are therefore the minimum possible water depth during the tidal cycle. "Drying heights" may also be shown on the chart, which are the heights of the exposed seabed at the lowest astronomical tide.

Tide tables list each day's high and low water heights and times. To calculate the actual water depth, add the charted depth to the published tide height. Depth for other times can be derived from tidal curves published for major ports. The rule of twelfths can suffice if an accurate curve is not available. This approximation presumes that the increase in depth in the six hours between low and high water is: first hour — 1/12, second — 2/12, third — 3/12, fourth — 3/12, fifth — 2/12, sixth — 1/12.

Biological aspects[link]

Intertidal ecology[link]

A rock, seen at low water, exhibiting typical intertidal zonation.

Intertidal ecology is the study of intertidal ecosystems, where organisms live between the low and high water lines. At low water, the intertidal is exposed (or ‘emersed’) whereas at high water, the intertidal is underwater (or ‘immersed’). Intertidal ecologists therefore study the interactions between intertidal organisms and their environment, as well as among the different species. The most important interactions may vary according to the type of intertidal community. The broadest classifications are based on substrates — rocky shore or soft bottom.

Intertidal organisms experience a highly variable and often hostile environment, and have adapted to cope with and even exploit these conditions. One easily visible feature is vertical zonation, in which the community divides into distinct horizontal bands of specific species at each elevation above low water. A species' ability to cope with desiccation determines its upper limit, while competition with other species sets its lower limit.

Humans use intertidal regions for food and recreation. Overexploitation can damage intertidals directly. Other anthropogenic actions such as introducing invasive species and climate change have large negative effects. Marine Protected Areas are one option communities can apply to protect these areas and aid scientific research.

Biological rhythms[link]

The approximately fortnightly tidal cycle has large effects on intertidal organisms. Hence their biological rhythms tend to occur in rough multiples of this period. Many other animals such as the vertebrates, display similar rhythms. Examples include gestation and egg hatching. In humans, the menstrual cycle lasts roughly a lunar month, an even multiple of the tidal period. Such parallels at least hint at the common descent of all animals from a marine ancestor.^[48]

Other tides[link]

When oscillating tidal currents in the stratified ocean flow over uneven bottom topography, they generate internal waves with tidal frequencies. Such waves are called internal tides.

Shallow areas in otherwise open water can experience rotary tidal currents, flowing in directions that continually change and thus the flow direction (not the flow) completes a full rotation in 12½ hours (for example, the Nantucket Shoals.^[49]

In addition to oceanic tides, large lakes can experience small tides and even planets can experience atmospheric tides and Earth tides. These are continuum mechanical phenomena. The first two take place in fluids. The third affects the Earth's thin solid crust surrounding its semi-liquid interior (with various modifications).

Lake tides[link]

Large lakes such as Superior and Erie can experience tides of 1 to 4 cm, but these can be masked by meteorologically induced phenomena such as seiche.^[50] The tide in Lake Michigan is described as 0.5 to 1.5 inches (13 to 38 mm)^[51] or 1¾ inches.^[52]

Atmospheric tides[link]

Atmospheric tides are negligible at ground level and aviation altitudes, masked by weather's much more important effects. Atmospheric tides are both gravitational and thermal in origin and are the dominant dynamics from about 80–120 kilometres (50–75 mi) above which the molecular density becomes too low to support fluid behavior.

Earth tides[link]

Earth tides or terrestrial tides affect the entire Earth's mass, which acts similarly to a liquid gyroscope with a very thin crust. The Earth's crust shifts (in/out, east/west, north/south) in response to lunar and solar gravitation, ocean tides, and atmospheric loading. While negligible for most human activities, terrestrial tides' semi-diurnal amplitude can reach about 55 centimetres (22 in) at the equator—15 centimetres (5.9 in) due to the sun—which is important in GPS calibration and VLBI measurements. Precise astronomical angular measurements require knowledge of the Earth's rotation rate and nutation, both of which are influenced by Earth tides. The semi-diurnal M₂ Earth tides are nearly in phase with the moon with a lag of about two hours.^{[citation needed]}

Some particle physics experiments must adjust for terrestrial tides.^[53] For instance, at CERN and SLAC, the very large particle accelerators account for terrestrial tides. Among the relevant effects are circumference deformation for circular accelerators and particle beam energy.^[54][55] Since tidal forces generate currents in conducting fluids in the Earth's interior, they in turn affect the Earth's magnetic field. Earth tides have also been linked to the triggering of earthquakes^[56] (see also earthquake prediction).

Galactic tides[link]

Galactic tides are the tidal forces exerted by galaxies on stars within them and satellite galaxies orbiting them. The galactic tide's effects on the Solar System's Oort cloud are believed to cause 90 percent of long-period comets.^[57]

Misapplications[link]

Tsunamis, the large waves that occur after earthquakes, are sometimes called tidal waves, but this name is given by their resemblance to the tide, rather than any actual link to the tide. Other phenomena unrelated to tides but using the word tide are rip tide, storm tide, hurricane tide, and black or red tides.

See also[link]

	Nautical portal
	Water portal
	Moon portal
	Earth sciences portal

Notes[link]

External links[link]

Wikiquote has a collection of quotations related to: Tides

Wikimedia Commons has media related to: Tides

• 150 Years of Tides on the Western Coast: The Longest Series of Tidal Observations in the Americas NOAA (2004).
• Eugene I. Butikov: A dynamical picture of the ocean tides
• Earth, Atmospheric, and Planetary Sciences MIT Open Courseware; Ch 8 §3
• Myths about Gravity and Tides by Mikolaj Sawicki (2005).
• Ocean Motion: Open-Ocean Tides
• Oceanography: tides by J. Floor Anthoni (2000).
• Our Restless Tides: NOAA's practical & short introduction to tides.
• Planetary alignment and the tides (NASA)
• Tidal Misconceptions by Donald E. Simanek.
• Tides and centrifugal force: Why the centrifugal force does not explain the tide's opposite lobe (with nice animations).
• O. Toledano et al. (2008): Tides in asynchronous binary systems
• Gif Animation of TPX06 tide model based on TOPEX/Poseidon (T/P) satellite radar altimetry
• Gaylord Johnson "How Moon and Sun Generate the Tides" Popular Science, April 1934
• Tide gauge observation reference networks (French designation REFMAR: Réseaux de référence des observations marégraphiques)

Tide predictions[link]

• NOAA Tide Predictions
• NOAA Tides and Currents information and data
• History of tide prediction
• Department of Oceanography, Texas A&M University
• Mapped, graphical and tabular tide charts for US displayed as calendar months
• Mapped, graphical US tide tables/charts in calendar form from NOAA data
• SHOM Tide Predictions
• UK Admiralty Easytide
• UK, South Atlantic, British Overseas Territories and Gibraltar tide times from the UK National Tidal and Sea Level Facility
• Tide Predictions for Australia, South Pacific & Antarctica
• Tide and Current Predictor, for stations around the world
• World Tide Tables
• Famous Tidal Prediction Pioneers and Notable Contributions

Physical oceanography – Waves and Currents Waves Airy wave theory Ballantine Scale Benjamin–Feir instability Boussinesq approximation Breaking wave Clapotis Cnoidal wave Cross sea Dispersion Infragravity waves Edge wave Equatorial waves Fetch Freak wave Gravity wave Internal wave Kelvin wave Luke's variational principle Mild-slope equation Radiation stress Rogue wave Rossby wave Rossby-gravity waves Sea state Seiche Significant wave height Sneaker wave Soliton Stokes boundary layer Stokes drift Surf wave Swells Tsunami Undertow Ursell number Wave base Wave–current interaction Wave height Wave power Wave setup Wave shoaling Wave radar Wave turbulence Waves and shallow water Shallow water equations Wind wave Wind wave model More... Circulation Atmospheric circulation Baroclinity Boundary current Coriolis effect Downwelling Eddy Ekman layer Ekman spiral Ekman transport El Niño-Southern Oscillation Geostrophic current Gulf Stream Halothermal circulation Humboldt Current Hydrothermal circulation Global circulation model Langmuir circulation Longshore drift Loop Current Maelstrom Ocean current Ocean dynamics Ocean gyre Rip current Thermohaline circulation Shutdown of thermohaline circulation Subsurface currents Sverdrup balance Whirlpool Upwelling GLODAP MOM POM WOCE More... Tides Amphidromic point Earth tide Head of tide Internal tide Lunitidal interval Perigean spring tide Rule of twelfths Slack water Spring/neap tide Tidal bore Tidal force Tidal power Tidal race Tidal range Tidal resonance Tide Tide gauge Tideline More...   Physical oceanography – Other Landforms Abyssal fan Abyssal plain Atoll Bathymetric chart Cold seep Continental margin Continental rise Continental shelf Contourite Hydrography Guyot Oceanic basin Oceanic plateau Oceanic trench Passive margin Seabed Seamount Submarine canyon Coastal geography More... Plate tectonics Black smoker Convergent boundary Divergent boundary Fracture zone Hydrothermal vent Marine geology Mid-ocean ridge Mohorovičić discontinuity Vine–Matthews–Morley hypothesis Oceanic crust Outer trench swell Ridge push Seafloor spreading Slab pull Slab suction Slab window Subduction Transform fault Volcanic arc More... Ocean zones Benthic Deep ocean water Deep sea Littoral Mesopelagic Oceanic zone Pelagic Photic Surf zone Sea level Current sea level rise Future sea level Sea-level curve DART GLOSS NOOS OSTM WGS Acoustics Ocean acoustic tomography Sofar bomb SOFAR channel Underwater acoustics Hydroacoustics Other Alvin Argo Benthic lander Color of water Marginal sea Mooring Ocean Ocean energy Ocean exploration Ocean observations Ocean pollution Ocean reanalysis Ocean surface topography Ocean thermal energy conversion Oceanography Pelagic sediments Sea surface microlayer Sea surface temperature Seawater Science On a Sphere Thermocline Underwater glider Water column World Ocean Atlas NODC More...

Template:The moon

Pirates of the Caribbean: On Stranger Tides is a 2011 adventure fantasy film and the fourth installment in the Pirates of the Caribbean series. Gore Verbinski, who had directed the three previous films, was replaced by Rob Marshall, while Jerry Bruckheimer again served as producer.

In the film, which draws inspiration from the novel On Stranger Tides by Tim Powers, Captain Jack Sparrow (Johnny Depp) is joined by Angelica (Penélope Cruz) in his search for the Fountain of Youth, confronting the infamous pirate Blackbeard (Ian McShane). The film was distributed by Walt Disney Pictures and was released in the US on May 20, 2011. It was released in Digital 3-D, IMAX 3D and 2D theatres.

Writers Ted Elliott and Terry Rossio first learned of Powers' novel during the back-to-back production of Dead Man's Chest and At World's End, and considered it a good starting point for a new movie in the series. Pre-production started after the end of the 2007–2008 Writers Guild of America strike, with Johnny Depp collaborating with the writers on the story design. Principal photography rolled for 106 days between June and November 2010, with locations in Hawaii, the United Kingdom, Puerto Rico, and California. Filming employed 3D cameras similar to those used in the production of the 2009 film Avatar, and ten companies were involved with the film's visual effects.

On Stranger Tides broke many box office records upon release, and it stands as the 9th highest-grossing film of all time worldwide when not adjusting for inflation. Critical reviews were mixed to negative, with the film receiving criticism over the script-writing, excessiveness, and lack of originality; positive mentions were given on the acting, directing and visuals.

Plot[link]

After a failed attempt to rescue his first mate, Joshamee Gibbs (Kevin McNally) in London, Captain Jack Sparrow (Johnny Depp) is brought before King George II (Richard Griffiths), who wants Jack to guide an expedition to the Fountain of Youth before the Spanish locate it. Heading the expedition is Jack's old nemesis, Captain Hector Barbossa (Geoffrey Rush), now a privateer in service to the Royal Navy after losing his leg and ship, the Black Pearl.

Jack escapes, but his father, Captain Teague (Keith Richards), finds him and warns Jack about the Fountain's tests. He also reveals that someone is impersonating Jack. The impostor is Angelica (Penélope Cruz), Jack's former lover and daughter of the ruthless pirate Blackbeard (Ian McShane), who practices voodoo magic and wields a magical sword that controls his ship.

Jack is taken aboard Blackbeard's ship, the Queen Anne's Revenge, and forced to lead the way to the Fountain and find two silver chalices that once belonged to Juan Ponce de León, both believed to be aboard his lost ship. The Fountain's water must be drunk simultaneously from the two chalices. The person drinking from the chalice containing a mermaid's tear has their life extended, while the other person dies, their life drained from their body and their remaining years 'donated' to the other. Meanwhile, Gibbs, having memorized and destroyed Jack's map, barters with Barbossa to guide him to the Fountain.

Blackbeard seeks the Fountain's power to circumvent his predestined fatal encounter with "a one-legged man," and sets a course for Whitecap Bay. There they are attacked by a vicious horde of mermaids, but Blackbeard captures one (Àstrid Bergès-Frisbey). Philip Swift (Sam Claflin), a captive missionary, falls in love with the mermaid and names her Syrena. Blackbeard then sends Jack to retrieve the chalices from de León's ship.

When Jack finds the grounded, decaying vessel, Barbossa is waiting inside and the Spanish are in possession of the chalices. However, Barbossa only seeks revenge against Blackbeard for capturing the Black Pearl, which forced Barbossa to amputate his own leg to escape. He and Jack join forces to defeat Blackbeard, then head to the nearby Spanish camp to steal the chalices. Meanwhile, Syrena, reciprocating Philip's love, is tricked into shedding a tear which Blackbeard collects, leaving her to die. Philip is forced to go with him. Jack returns with the chalices and Gibbs, with whom he had reunited while assisting Barbossa. Jack and Blackbeard bargain for Jack's confiscated magical compass and Gibbs' release. In return, Jack vows to give Blackbeard the chalices and lead him to the Fountain; Blackbeard agrees and Gibbs departs with the compass.

At the Fountain, Blackbeard and his crew are attacked by Barbossa, and then by the Spanish, there to destroy the Fountain, their king believing its power is an abomination against God. A battle ensues and Barbossa stabs Blackbeard with a poison-laced sword. Angelica accidentally cuts herself while removing it from Blackbeard. Barbossa claims Blackbeard's magical sword and assumes command, leaving with Blackbeard's crew. Meanwhile, Philip, though mortally wounded, escapes and returns to free Syrena. After finding the chalices that the Spaniard had tossed into deep water, Syrena gives them to Jack, then retrieves the dying Philip and takes him underwater.

With Blackbeard and Angelica wounded, Jack brings the chalices to them and tries to convince Angelica to drink from the one with the tear, but Blackbeard asks his daughter to sacrifice herself. Angelica agrees and drinks. Knowing that the self-serving Blackbeard would sacrifice his daughter, Jack lied about which chalice contained the tear. Blackbeard's body is drained by the waters of the Fountain and destroyed. Although Angelica admits her love for Jack, he strands her on an island, knowing that she may want to avenge her father's death. Barbossa, who now captains the Queen Anne's Revenge, quits being a privateer and returns to piracy. Jack finds Gibbs, who has used the compass to locate the shrunken Black Pearl and is shown to be in possession of all ships Blackbeard had shrunken in bottles. Hoping to bring the Black Pearl to its original size, the two head off into the sunset, determined to continue living a pirate's life.

In a post-credits scene, Angelica, still on the island, finds Blackbeard's voodoo doll of Jack, which has washed ashore, to which she reacts with a grin.

Cast[link]

Top to bottom: Johnny Depp and Geoffrey Rush who reprised their roles from the previous films as Captain Jack Sparrow and Captain Hector Barbossa respectively.

• Johnny Depp as Captain Jack Sparrow, former captain of the Black Pearl and the main protagonist.
• Geoffrey Rush as Captain Hector Barbossa, Jack's nemesis and former member of the Black Pearl.
• Penélope Cruz as Angelica, Jack's former love interest.
• Ian McShane as Edward "Blackbeard" Teach, captain of the Queen Anne's Revenge and the main antagonist.
• Kevin McNally as Joshamee Gibbs
• Sam Claflin as Philip Swift
• Àstrid Bergès-Frisbey as Syrena
• Greg Ellis as Lt. Cmdr. Theodore Groves
• Damian O'Hare as Lieutenant Gillette
• Stephen Graham as Scrum
• Óscar Jaenada as The Spaniard, King Ferdinand's most trusted agent
• Gemma Ward as Tamara
• Richard Griffiths as King George II of Great Britain
• Keith Richards as Captain Teague
• Judi Dench as a noblewoman
• Robbie Kay as the Cabin boy
• Derek Mears as the Master-at-Arms
• Deobia Oparei as the Gunner
• Danny Le Boyer as Yeoman
• Ian Mercer as the Quartermaster
• Sebastian Armesto as King Ferdinand of the Spanish Empire
• Anton Lesser as Lord John Carteret
• Roger Allam as Henry Pelham, Prime Minister of Great Britain
• Paul Bazely as Salaman, an Indian crew member of the Queen Anne's Revenge

Production[link]

Development[link]

Shortly before the premiere of At World's End, Jerry Bruckheimer stated it was the end of the trilogy, but the idea of a spin-off was still possible.^[3] After the film's successful opening weekend, Dick Cook, former Chairman of the Walt Disney Studios, said he was interested in a fourth installment.^[4] Ted Elliott and Terry Rossio had started working on a script in 2007, but they were interrupted by the 2007–2008 Writers Guild of America strike, and only resumed in mid-2008.^[5] On September 25, 2008, during a Disney event at the Kodak Theater, Cook and Johnny Depp, in full Captain Jack Sparrow costume, announced that a fourth Pirates movie was in development.^[6]

In June 2009 Bruckheimer indicated Disney would prefer the fourth installment of Pirates to be released before The Lone Ranger film, which he, Johnny Depp, Ted Elliott, and Terry Rossio had been working on for release on May 20, 2011. He hoped Gore Verbinski would return to direct the fourth film, as his BioShock film adaptation had been put on hold.^[7] As Verbinski was unavailable due to his commitment with Rango the same year, Bruckheimer suggested Rob Marshall, who he considered a "premiere filmmaker", stating that "Every film [Marshall] made I thought was unique and different."^[8] On July 21, 2009, Marshall accepted the job, because of the "whole new story line and set of characters. It felt new, and that was important to me." ^[5] Marshall said the film provided him a long-awaited opportunity to work with Depp, and that his directing was helped by past experience as a choreographer – "the action sequences felt like big production numbers."^[9] On September 11, 2009, at Disney's D23 convention, the title was announced as Pirates of the Caribbean: On Stranger Tides.^[10] Marshall visited the Pirates of the Caribbean ride in Disneyland for inspiration, eventually paying homage with a skeleton holding a magnifying glass in Ponce de Leon's ship. An appearance of "Old Bill", the pirate who tries to share his rum with a cat, was also filmed but cut.^[11]

Cook resigned in September 2009 after working for Disney for over 38 years.^[12] Depp's faith in Pirates of the Caribbean: On Stranger Tides was somewhat shaken after the resignation, with Depp explaining that "There's a fissure, a crack in my enthusiasm at the moment. It was all born in that office".^[13] Depp also explained Cook was one of the few who accepted his portrayal of Jack Sparrow: "When things went a little sideways on the first Pirates movie and others at the studio were less than enthusiastic about my interpretation of the character, Dick was there from the first moment. He trusted me".^[13]

Writing[link]

During production of Dead Man's Chest and At World's End, writers Ted Elliott and Terry Rossio discovered Tim Powers' 1987 novel On Stranger Tides, which they considered a good foundation on which to base "a new chapter" in the Pirates series.^[8] Disney bought the rights to the novel in April 2007.^[14] Rossio stated that he and Elliot had considered using Blackbeard and the Fountain of Youth in the story before reading the book, "but whenever you say those words, Powers' novel comes to mind. There was no way we could work in that field without going into territory Tim had explored." However, they denied that it would be a straight version of the novel: "Blackbeard came from the book, and in the book there is a daughter character, too. But Jack Sparrow is not in the book, nor is Barbossa. So I wouldn't call this an adaptation."^[5] Rossio declared the script was written to be a standalone film, "kind of a James Bond sort of thing", instead of the "designed to be a trilogy" structure of the previous installments.^[15] They hoped to "design a story that would support new characters," as characters such as Will Turner would not return.^[16] Bruckheimer added that there was a decision to "streamline the story a little bit, make it a little simpler and not have as many characters to follow", as the number of characters and subplots in At World's End caused the film to have an unwieldy length.^[8] The duo decided to employ another sea myth alluded in the previous episodes: mermaids,^[15] which are briefly referenced in the book. The mermaids' role expanded in the script, which included a vast attack sequence.^[16]

Depp was deeply involved with the story design, frequently meeting the writers to show what he was interested in doing, and in the words of Rossio, being "involved in coming up with story lines, connecting characters, creating moments that we would then fashion, shape and then go back."^[15] Among Depp's suggestions were turning Phillip into a missionary, and having a Spanish contingent following the protagonists. Afterwards, Rob Marshall and executive producer John DeLuca met Rossio and Elliot, and did alterations of their own, including building the female lead.^[16]

Casting[link]

Depp signed on to return as Captain Jack Sparrow in September 2008, saying that he would come back if the script was good.^[6] Almost a year later, Disney announced that Depp would be paid $55.5 million for his role, realising that without him the franchise would be "dead and buried."^[17] Geoffrey Rush expressed interest in returning to his role as Barbossa,^[18] and Bruckheimer later confirmed his presence.^[19] Rush was positive on Barbossa having lost a leg, as he considered the disability made him "angrier, more forceful and resilient as a character", and had to work with the stunt team for an accurate portrayal of the limp and usage of cane, particularly during swordfighting scenes.^[20] While the production team considered a prop pegleg to be put over Rush's leg, the tight schedule caused it to be replaced with a blue sock that was replaced digitally, with a knob on the shoe to give Rush a reference for his walk.^[21] Three other actors from the previous films returned, Kevin McNally as Joshamee Gibbs, Greg Ellis as Lt. Theodore Groves,^[22] and Damian O'Hare as Lt. Gilette.^[23] Keith Richards also had a cameo, reprising his role as Captain Teague from At World's End; he and Depp tried to persuade Mick Jagger to audition for the part of a pirate elder.^[24] Previous cast members Orlando Bloom and Keira Knightley stated that they would not reprise their roles, as they wanted to be involved in different films. They both thought the storyline involving their characters had gone as far as it could.^[25][26][27] On February 5, 2010, Mackenzie Crook also announced he would not be reprising his role of Ragetti, stating, "They haven't asked me. But actually I don't mind that at all. I'm a fan of the first one especially and I think the trilogy we've made is great. I'd almost like them to leave it there."^[28]

New cast members include Ian McShane, who plays the notorious pirate and primary antagonist of the film, Blackbeard, and Penélope Cruz, who plays Angelica, Jack Sparrow's love interest.^[19] According to Marshall, McShane was chosen because "he can play something evil but there’s always humor behind it as well", and the actor accepted the job due to both the "very funny and charming" script and the opportunity to work with Marshall.^[29] The beard took one hour and a half to get applied, and McShane likened the character's costume to "a real biker pirate – it’s all black leather.”^[30] Marshall said Cruz was the only actress considered for the role, as she fit the description as "an actress who could not only go toe to toe with Johnny and match him, but also needed to be all the things that Jack Sparrow is in a way. She needed to be funny and clever and smart and crafty and beautiful",^[9] and invited her for the role as they wrapped the production of Nine.^[21] The actress spent two months working out and learning fencing for the role.^[31] During filming, Cruz discovered she was pregnant, leading the costume department to redesign her wardrobe to be more elastic,^[21] and the producers to hire her sister Mónica Cruz to double for Penélope in risky scenes.^[32] Depp recommended Stephen Graham, who worked with him in Public Enemies, to play Scrum, a Machiavellian pirate and sidekick to Jack Sparrow,^[33][34] and Richard Griffiths for the role of King George II, as Depp was a fan of Griffiths' work on Withnail and I.^[21] Sam Claflin, a recent drama school graduate with television experience, was chosen to play the missionary Philip,^[35] and British actor Paul Bazely also joined the cast.^[36] Spanish news website El Pais reported that the film had four Spanish actors: Cruz, Bergès-Frisbey, Óscar Jaenada, and Juan Carlos Vellido.^[37] Jaenada was picked for both his work in The Losers and a recommendation by Cruz.^[38]

Casting for mermaids required the actresses to have natural breasts—no implants. As Bruckheimer explained to EW, "I don’t think they had breast augmentation in the 1700s, [...] So it’s natural for casting people to say, ‘We want real people.'"^[39] Marshall invited Spanish-French actress Àstrid Bergès-Frisbey to play Syrena after seeing her in a French magazine article on up-and-coming actresses.^[20] Bergès-Frisbey had to take lessons of English, swimming and breath control for the role.^[22] The rest of the mermaid portrayers, such as Australian supermodel Gemma Ward,^[40] were chosen for having "exotic sense, an otherworldly sensibility, but also under those layers a deadly quality", according to Marshall, and had to take swimming lessons to learn movements such as the dolphin and eggbeater kicks.^[41]

Filming[link]

Principal photography began on June 14, 2010, in Hawaii.^[42][16] Filming was moved to California in August 2010,^[43] primarily at the Long Beach shore^[29] and a recreation of Whitecap Bay done in the Universal Studios backlot,^[16] as the original Hawaiian location on Halona Cove was plagued with strong tides.^[20] After a brief shoot in Puerto Rico,^[29] with locations in both Palomino Island and the Fort of San Cristóbal in San Juan,^[44] production moved to the United Kingdom in September, where principal photography wrapped on November 18 after 106 days of shooting.^[16] Locations included Hampton Court Palace in London,^[21] Knole House in Kent,^[29] and Old Royal Naval College at Greenwich.^[45] Interiors were shot at London's Pinewood Studios, and a replica of a 17th century London street was built on the backlot alongside the soundstages.^[46][29] The producers also considered using New Orleans as a location.^[47] In October, security was breached at the UK site when a celebrity impersonator gained access to filming at the Old Royal Naval College by dressing up as Captain Jack.^[48]

After the joint production of Dead Man's Chest and At World's End cost over $300 million, Disney decided to give a lower budget to the fourth installment.^[1] Many costs had to be cut, including moving primary production to Hawaii and London, where tax credits are more favorable, and having a shorter shooting schedule and fewer scenes featuring special effects compared to At World's End.^[49] The tighter schedule—according to Bruckheimer, "We had a 22-week post, and for a picture like this, with almost 1,200 visual effects shots, it's usually 40 weeks"—meant that Marshall supervised editing of sequences during filming.^[16]

Jerry Bruckheimer said the decision to film in 3D was made due to its being "immersive filmmaking; I think it makes you part of the actual filming because you’re part of the screen." Bruckheimer described it as the first major "exterior movie" to be shot in 3D, as Avatar was mostly done in sound stages.^[8] At first Marshall was not much interested in 3D, but the director eventually considered it a film that could benefit from the format. "You are on an adventure and with the 3D experience you are inside that adventure."^[9] While the original plan was to add 3D effects during post-production, the decision was made to shoot digitally with 3D cameras. Only one sequence was shot conventionally and needed a 3D conversion.^[8] The cameras were improved versions of the ones James Cameron developed for Avatar, which were made more compact for extra mobility. This meant the cameras could be brought into locations such as the Hawaiian jungle.^[50]

The Queen Anne's Revenge was built atop the Sunset, the same ship used to depict the Black Pearl in previous installments. On February 2010, the Sunset was sailed from Long Beach to a shipyard in Hawaii for the reforms, where a big concern was to make it imposing, with three stories, without sacrificing actual seakeeping. Given Blackbeard was meant to be the meanest pirate to appear in the series, the look for the Queen Anne's Revenge was ominous, with sails dyed blood red, various elements on fire, and a decoration based on skulls and bones (drawing inspiration from the Sedlec Ossuary in Czech Republic). Damage from cannon fire was also added to show that "not only Blackbeard was a dying man, but his ship is also a dying ship". The ship's figurehead also drew inspiration from Blackbeard's pirate flag.^[51] The replica ship HMS Surprise was used for Barbossa's ship, the HMS Providence,^[52] and all the scenes aboard the Providence were shot on the Long Beach shore as the Surprise could not be sailed to Hawaii.^[21] Over 50 designs were considered for the Fountain of Youth, with the final one representing a temple built by an ancient civilization around the Fountain, which itself was located in a round rocky structure to represent "the circle of life". The locations leading up to the Fountain were shot in the Hawaiian islands of Kauai and Oahu, but the Fountain itself was built at the 007 Stage on Pinewood.^[53]

Effects[link]

On Stranger Tides employed 1,112 shots of computer-generated imagery,^[16] which were done by ten visual effects companies.^[54] Cinesite visual effects supervisor Simon Stanley-Clamp claimed that the most difficult part was doing the effects in 3D: "Rotoscoping is tricky. Cleaning up plates is double the work, and tracking has to be spot on."^[45] The lead companies, with over 300 effects each, were Industrial Light & Magic—responsible for, among others, the mermaids and most water effects^[55]—and Moving Picture Company, who created digital ships and environment extensions, such as changing weather and designing cliffs and waterfalls.^[56] Filming the mermaids involved eight model-actresses, who portrayed them outside the water, as well as 22 synchronized swimming athletes and a group of stuntwomen, both of whom wore motion capture suits to be later replaced by digital mermaids. Mermaid corpses were depicted by plaster models.^[41][29] The design tried to avoid the traditional representations of mermaids in paintings and literature, instead going for a scaly body with a translucent membrane inspired by both jellyfish and the fabric employed in ballet tutus. To make the mermaids more menacing underwater, the faces of the actresses had some digital touch-ups on the underwater scenes, adding sharper teeth and a shimmery fish scale quality on the skin.^[57] ILM also handled Blackbeard's death, where Ian McShane's actual performance was covered by digital doubles which turned him into a "boiling mass of blood and clothing", and a hurricane-like formation that represented "the waters of the Fountain taking his life".^[53] Cinesite handled the recreation of London and Barbossa's peg leg,^[45] CIS Hollywood did 3D corrections and minor shots, and Method Studios created matte paintings.^[58]

Music[link]

The film's score was written by Hans Zimmer, who had worked in all of the previous entries in the franchise; being the main composer for the second and third installments.^[59] Zimmer said that he tried to incorporate a rock n' roll sound, as he felt "pirates were the rock 'n' rollers of many, many years ago",^[60] and Spanish elements, which led to a collaboration with Mexican guitarists Rodrigo y Gabriela and a tango song written by Penélope Cruz's brother Eduardo.^[61] American composer Eric Whitacre contributed several choir-based cues,^[61][62] as well as regular assistant Geoff Zanelli.^[59]

Release[link]

Penélope Cruz and Johnny Depp promoting the film at the 2011 Cannes Film Festival.

On January 6, 2010, Disney announced that the film would be released in the United States and Canada on May 20, 2011, following Columbia Pictures' announcement of a delay in the Spider-Man reboot and Paramount Pictures slating Thor for May 6, 2011.^[63] The film was released in IMAX 3D, as well as traditional 2D and IMAX format,^[64][65] with Dolby 7.1 surround sound.^[66]

The world premiere of On Stranger Tides was on May 7, 2011, at a premium ticket screening at Disneyland in Anaheim, California, home of the original Pirates of the Caribbean ride that inspired the film series. Many of the film's stars were in attendance. Two other early screenings followed, one in Moscow on May 11,^[67] and another during the Cannes International Film Festival on May 14.^[68] The international release dates fell within May 18 and May 20, with opening dates in the United Kingdom on May 18, in Australia on May 19, and in North America on May 20.^{[69][70][71][72]} The film was released on a then-record 402 IMAX screens, 257 screens in North America, and 139 in other territories.^[73] The total number of theaters was 4,155 in North America and 18,210 worldwide.^[74][75]