text:
Flowers in the Rain
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For the album by Mad at the World, see Flowers in the Rain (album).
"Flowers in the Rain"
Single by The Move
from the album Move
B-side
"(Here We Go Round) the Lemon Tree"
Released
August 1967
Format
7" single
Recorded
6 July 1967
Studio
Advision Sound Studios, London
Genre
Psychedelic pop
Length
2:29 (original version)
2:41 (2007 remastered version)
Label
Regal Zonophone (UK)
A&M (US)
Songwriter(s)
Roy Wood
Producer(s)
Denny Cordell
The Move singles chronology
"I Can Hear the Grass Grow"
(1967) "Flowers in the Rain"
(1967) "Fire Brigade"
(1968)
"I Can Hear the Grass Grow"
(1967) "Flowers in the Rain"
(1967) "Fire Brigade"
(1968)
"Flowers in the Rain" is a song by English rock band The Move. The song was released as a single and reached number two in 1967 on the UK Singles Chart, and number four in Ireland.
It achieved its own place in pop history by being the first record[1] to be played on Radio 1 when the station was launched in 1967 (though technically Johnny Dankworth's "Beefeaters" was the first track to be heard, since Tony Blackburn chose it as the theme tune for his Daily Disc Delivery,[1] and so it was heard before "Flowers in the Rain"[2]). "Flowers in the Rain" was also the last single by The Move to have Carl Wayne on lead vocals before Roy Wood took over as the band's lead vocalist for "Fire Brigade".
The distinctive instrumental arrangement, including oboe, clarinet, cor anglais and French horn, was suggested by assistant producer Tony Visconti.[1]
Contents
[hide]
1 Promotional stunt
2 Personnel
3 Covers
4 References
Promotional stunt[edit]
In a promotional stunt, for the record—typical of the band's manager Tony Secunda—a postcard was released with a cartoon of a naked Harold Wilson, linking him to his secretary Marcia Williams. Wilson sued, and the High Court ordered that all royalties from the song were donated to a charity of Wilson's choice. This legal arrangement remains in force to this day and is thought to have cost the group millions of pounds in royalties over the years. During the single's chart success, most of the money went to the Spastics Society and Stoke Mandeville Hospital. In the 1990s, The Observer newspaper reported the royalties had exceeded £200,000 and found that The Harold Wilson Charitable Trust had extended the range of beneficiaries to include, among others, the Oxford Operatic Society, Bolton Lads Club and the Jewish National Fund for Israel.[1]
Personnel[edit]
Carl Wayne – lead vocals
Roy Wood – guitars, lead vocals
Trevor Burton – guitars
Ace Kefford – bass
Bev Bevan – drums
Covers[edit]
The song has been covered by Nancy Sinatra. The Kaiser Chiefs also covered this for the Radio 1 Established 1967 CD.[3] In 1997 it was covered by Arjen Anthony Lucassen for his anonymously released album Strange Hobby.
On 25 September 2007, BBC Radio 4 featured a programme called The Story of Flowers in the Rain, hosted by Tony Blackburn, on the court action and its related history, to celebrate the 40th anniversary of the song.[4] In the programme, the band said that although they still play the song regularly, they are beginning to get fed up with it.
References[edit]
^ Jump up to: a b c d "Flower Power". BBC News. 24 August 2007. Retrieved 2007-08-25.
Jump up ^ Another school of thought cites Julie Andrews' "The Sound of Music" as the first track since this was played at 5:30am when the new Radio One frequency opened up with a shared programme, heard simultaneously on Radio Two, hosted by Paul Hollingdale (The Weekly News, Issue 7,946, 29 September 2007)
Jump up ^ "Radio 1 Established 1967". BBC Radio 1. September 2007. Retrieved 20 February 2013.
Jump up ^ "The Story of Flowers in the Rain". BBC Radio 4. 25 September 2007. Retrieved 20 February 2013.
[hide]
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The Move
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Studio albums
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Related articles
Electric Light Orchestra
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Death in Paradise (TV series)
From Wikipedia, the free encyclopedia
Jump to navigation Jump to search
Death in Paradise
Genre
Crime drama
Detective fiction
Created by
Robert Thorogood
Starring
Ben Miller
Sara Martins
Danny John-Jules
Gary Carr
Don Warrington
Élizabeth Bourgine
Kris Marshall
Joséphine Jobert
Tobi Bakare
Sally Bretton
Ardal O'Hanlon
Shyko Amos
Composer(s)
Magnus Fiennes
Country of origin
United Kingdom
France
Original language(s)
English
No. of series
7
No. of episodes
56 (list of episodes)
Production
Executive producer(s)
Tony Jordan
Klaus Zimmermann
Belinda Campbell
Producer(s)
Matthew Bird
Tim Key
Tim Bradley
Production location(s)
Guadeloupe
Running time
60 minutes
Production company(s)
Red Planet Pictures
Atlantique Production
Kudos
France Télévisions
Release
Original network
BBC One
BBC One HD
Picture format
16:9
Audio format
Stereo
Original release
25 October 2011 (2011-10-25) – present
External links
Website
Death in Paradise is a British-French crime drama television series created by Robert Thorogood, starring Ben Miller (series 1–3), Kris Marshall (series 3–6) and Ardal O'Hanlon (series 6–present). The programme is a joint UK and French production filmed on the French Caribbean island of Guadeloupe and broadcast on BBC One in the United Kingdom and France 2 in France. Death in Paradise has enjoyed high ratings,[1] leading to repeated renewals.[2] A seventh series began broadcasting on 4 January 2018[3], with an eighth for 2019 already commissioned, with O'Hanlon and Jobert confirmed to return[4].
Contents
1 Synopsis
2 Episodes
3 Format
4 Setting
4.1 Saint Marie
4.2 Other locations
5 Characters
5.1 Main
5.2 Recurring
6 Production
7 Reception
7.1 Viewing figures
7.2 Critical response
7.3 Awards
8 DVD release
9 Broadcast
10 Music
10.1 Theme music
10.2 Soundtrack
11 Novels
12 Notes
13 References
14 External links
Synopsis[edit]
British detective Richard Poole (Ben Miller) is assigned to investigate the murder of a British police officer on the fictional Caribbean island of Saint Marie.[5] After he successfully finds the murderer, he is reluctantly required by his supervisors to replace the victim and stay on as the detective inspector (DI) of the island, solving new cases as they appear, and being the object of many fish-out-of-water jokes.[6] At the start of Series 3, Poole is killed and maladroit London detective Humphrey Goodman (Kris Marshall) arrives to investigate the death of his strait-laced predecessor. He then stays in the job as chief investigator on the island. In the second half of Series 6, he resigns so he can stay in London with his new girlfriend Martha Lloyd. His replacement on Saint Marie is DI Jack Mooney, played by Ardal O'Hanlon.
Episodes[edit]
Main article: List of Death in Paradise episodes
Series
Episodes
Originally aired
Ave. UK viewers
(millions)[7]
First aired
Last aired
1 8 25 October 2011 (2011-10-25) 13 December 2011 (2011-12-13) 5.89
2 8 8 January 2013 (2013-01-08) 26 February 2013 (2013-02-26) 7.67
3 8 14 January 2014 (2014-01-14) 4 March 2014 (2014-03-04) 8.46
4 8 8 January 2015 (2015-01-08) 26 February 2015 (2015-02-26) 9.03
5 8 7 January 2016 (2016-01-07) 25 February 2016 (2016-02-25) 8.67
6 8 5 January 2017 (2017-01-05) 23 February 2017 (2017-02-23) 9.10
7 8 4 January 2018 (2018-01-04) 22 February 2018 (2018-02-22) 8.34
Format[edit]
While Death in Paradise has continued to be in the top three most popular programmes on British television, critics have called the crime drama "unremarkable" and "an undemanding detective show, with nice Caribbean scenery".[8] The show is known for its formulaic approach to its plots[9] with each episode roughly the same in both style and narrative structure.
Each episode begins with a pre-credits sequence showing the events leading up to a murder, and often the discovery of the body afterwards; this sequence also serves to introduce that particular episode's guest characters.[10] The police force of Saint Marie are subsequently informed of the murder, preliminary investigations and interviews take place to establish the suspects and photographs of the suspects and crime scene are placed on the whiteboard at police headquarters.[11]
Often towards the end, the lead DI will have a moment of realisation, perhaps brought on by something that someone says or does or by some occurrence. In this moment, the how, why, and who of the murder are comprehended by the DI, but are not revealed to the audience. The suspects are then all gathered together and the DI talks through the evidence; often, flashbacks are used to show what happened. The murderer and the motive are revealed in the dénouement of the episode.[12]
Normally, each episode ends with a comedic scene or a celebratory trip by the police force to Catherine's bar.[13] The final episode of most series has included a subplot wherein the lead DI is tempted to return to the UK by the prospect of a job offer or personal relationship, but in the end, he decides to remain on the island. This format was subverted in the sixth series when the two-part storyline in the fifth and sixth episodes saw the team travel to London to follow up on a current case, resulting in then-lead detective Humphrey Goodman deciding to remain to be with his new girlfriend; D.I. Jack Mooney travelled back to Saint-Marie, initially as a holiday, but decided to remain as the new detective inspector of the island in the series finale.
Setting[edit]
Saint Marie[edit]
Main article: Saint Marie (fictional island)
Death in Paradise is set on the fictional Caribbean island of Saint Marie, described in Episode 3.3 as a "pretty island" that is "situated in the Eastern Caribbean Sea" and "one-tenth the size of its north-west neighbour Guadeloupe"; this would make Saint Marie about 63 square miles (160 km2) in size. Saint Marie is a British Overseas Territory, but about 30% of its people are French, due to previous history, with the language still widely spoken.
The back-story appears to be a blend of two real-world islands near to Guadeloupe, with size and location aligning with Marie-Galante and history and language aligning with Dominica.
In the TV show, the fictional Saint Marie island has a volcano, rainforest, sugar plantations, a fishing harbour, an airport, a university, a convent, approximately 100 public beaches and a Crown Court. It also has its own newspaper, The Saint Marie Times. Honoré, the main town, has a leisure/commercial marina, market, bars, and restaurants as well as the police station. The neighbouring town to Honoré is named as Port Royal. Saint Marie's main economic ties are to Guadeloupe, the UK, and France. The island's main religions are Catholicism and Voodoo, with several religious festivals featuring in the programme, including the Saint Ursula Festival (in reality, a major festival of the Virgin Islands) and some Voodoo festivals.
Other locations[edit]
Episode 3.7 is largely set on an islet just off Saint Marie; it is privately owned and relatively small. This episode was actually filmed on the island of Kahouanne, around 1.2 miles (1.9 km) off the north-west coast of Guadeloupe where the series is normally filmed. It can often be seen in the background from a beach on Saint Marie.
Episodes 6.5 and 6.6 are largely set in London when DI Goodman, DS Cassell and Officer Myers form a liaison team with future lead DI Jack Mooney in order to track down suspects in a murder investigation in Saint Marie, and later to investigate the murder of one of the suspects.
Characters[edit]
See also: List of Death in Paradise characters
Main[edit]
Character
Actor
Position
Series
1
2
3
4
5
6
7
8
Richard Poole Ben Miller DI Main Guest
Camille Bordey Sara Martins DS Main
Dwayne Myers Danny John-Jules Officer Main
Fidel Best Gary Carr Officer/Sergeant Main
Selwyn Patterson Don Warrington Commissioner Main
Catherine Bordey Élizabeth Bourgine Restaurateur, Mayor (Series 7-) Recurring Main
Humphrey Goodman Kris Marshall DI Main
Florence Cassell Joséphine Jobert Sergeant/DS Main
JP Hooper Tobi Bakare Officer Main
Martha Lloyd Sally Bretton Guest Main
Jack Mooney Ardal O'Hanlon DI Main
Ruby Patterson Shyko Amos Officer Main
The original team: Left-to-right: Sara Martins, Danny John-Jules, Gary Carr and Ben Miller
Recurring[edit]
Character
Actor
Years
Series
Aidan Miles Adrian Dunbar 2011 1.7–1.8
Sally Goodman Morven Christie 2014 3.1a, 3.8
Martin Goodman, QC James Fox 2015 4.7a–4.8
Rosey Hooper (née Fabrice) Fola Evans-Akingbola[14][15] 2016 5.3, 5.5–5.6, 5.8
Nelson Myers Ram John Holder 2017-2018 6.5–6.6, 7.7–7.8
Siobhan Mooney Grace Stone 2017-2018 6.6–7.1
Darlene Curtis Ginny Holder 2018 7.3–7.5, 7.7
^a Made a voice cameo in this episode.
Danny John-Jules (who plays Officer Dwayne Myers) will not be returning for series eight and will be replaced by actress Shyko Amos playing Officer Ruby Patterson, the niece of the commissioner. [16] John-Jules cited his reason for exiting the show as wanting to “leave on a high".[17]
Production[edit]
Deshaies' church is right next to the fictional "Honoré police station".
The series is filmed on the French island of Guadeloupe in the Lesser Antilles, mainly in the commune of Deshaies (which doubles for the town of Honoré on the fictional island of Saint Marie), with the help of the Bureau d’accueil des tournages de la Région Guadeloupe.[18] The site of the Honoré police station is a church hall in Deshaies with the priest's office appearing as the incident room.[19]
Miller left the series at the start of series 3, as he felt he was spending too much time away from his family since his wife was unable to join him on the island during production. Marshall's family joined him on the island during his first three six-month shoots and his son Thomas enrolled at a local school. When his family did not join him during the filming of the sixth season, following the birth of his baby daughter Elsie, it left him feeling "bereft and empty" and he quit the show.[20] From episode 7 of the sixth season the lead role was taken by Ardal O'Hanlon playing DI Jack Mooney, a London colleague.[21]
Reception[edit]
Viewing figures[edit]
Regarding British TV ratings, Death in Paradise has gained in popularity over time.
Series 1 (2011) has been the least-watched to date, averaging 5.89 million viewers, with the 5.3 million viewers for the sixth episode, “An Unhelpful Aid” the lowest the show has had. Even so, each episode was among the top five most-watched programmes of the day, and in the top forty most-watched programmes of the week.
Series 2 (2013) averaged 7.67 million viewers, almost 2 million more than the previous series. Each episode was among the top two most-watched programmes of the day, and in the top fifteen most-watched programmes of the week.
Series 3 (2014) averaged 8.46 million viewers. Each episode was among the top two most-watched programmes of the day, and in the top ten most-watched programmes of the week.
Season 4 (2015) averaged 9.03 million viewers. Based on consolidated figures, each episode was among the top three most-watched programmes of the day, and in the top ten most-watched programmes of the week.
Season 5 (2016) averaged 8.67 million viewers. Based on consolidated figures, each episode was the most-watched programme of the day, and in the top four most-watched programmes of the week.
Season 6 (2017) has been the most-watched so far, averaging 9.1 million viewers. The season premiere, “Erupting in Murder” is the most-watched episode of the show to date with 9.81 million viewers. Based on consolidated figures, each episode of Series 6 was the most-watched programme of the day, and in the top four most-watched programmes of the week.
Series 7 (2018) averaged 8.34 million viewers. Based on consolidated figures, each episode was the most-watched programme of the day, and in the top ten most-watched programmes of the week.[22]
Critical response[edit]
The series has received mixed reviews from critics, with most criticism directed towards its formulaic structure. The first series was praised for its refreshing style and setting. Kris Marshall's introduction at the start of series 3 was particularly well received, with Rebecca Smith of The Daily Telegraph citing Marshall as a "winning addition" to the cast.[23] The series 4 premiere was described as "a little piece of escapism" and was generally praised. Mark Monahan of The Daily Telegraph criticised the laid-back tone of the series, calling it too methodical with nothing unique about it besides the setting.[24]
Awards[edit]
Red Planet Pictures was nominated for, and won, the "Diversity in a Drama Production Award" for Death In Paradise. Sara Martins, Danny John-Jules, Don Warrington and Tobi Bakare collected the award at a ceremony supported by the BBC and ITV that took place on 15 February 2015.[25]
DVD release[edit]
Series
Region 2
Region 1
Region 4
Discs
Extras
1 8 October 2012[26] 17 June 2014[27] 2 August 2012 [28] 2 N/A
2 4 March 2013 16 September 2014[29] 3 July 2013 [30] 3 N/A
3 10 March 2014 5 May 2015[31] 25 May 2014 [32] 3 The Making of Death in Paradise on disc three. Seven short insights into the making of Death in Paradise.
4 2 March 2015[33] 5 July 2016[34] 18 March 2015 [35] 3 N/A
5 29 February 2016 13 December 2016[36] 16 March 2016 [37] 3 The Making Of Death In Paradise
Creating The Puzzle
Harry The Lizzard
Tour Of Honoré Police Station
The Vehicles
1–5 29 February 2016 N/A 16 March 2016 [38] 14 same extras that were on series 3 and 5 (no extra were made for series 1–2 and 4)
6 27 February 2017 12 December 2017[39] 29 March 2017 [40] 3 N/A
1–6 N/A N/A 29 March 2017 [41] 17 same extras that were on series 3 and 5
7 26 February 2018 N/A 14 March 2018 [42] 3
1–7 N/A N/A 14 March 2018 [43] 20
Broadcast[edit]
In the U.K., all series were shown on BBC One. The first series was broadcast in late 2011. The second series was broadcast in January 2013, with subsequent series filling the same January slot; all series were shown in a 9:00–10:00 pm slot.[a] The series has also been shown on repeat on the Alibi channel, although with each episode missing the pre-intro sequence and a few expendable scenes due to the need for adverts on Alibi.
In France the programme is broadcast on France Ô.
In the U.S., many, but not all, member stations of PBS broadcast Death In Paradise. Series 1 and 2 were broadcast in the San Francisco Bay Area on KQED Mystery Night in 2013.[44] Series 1 aired in January and February 2013 and series 2 aired in April and May 2013.
In the New England area, WGBH-TV started airing Series 1 and 2 in 2013. Other PBS stations that air the programme as of 2016 include WPBA, WLIW, WTTW, KAET, KUAT, KUHT Houston, and WNED, among others. In Seattle-Tacoma, WA area broadcast on KBTC TV (PBS), Seasons 1-7 on Friday evenings with the current season aired April-May[45].
In Australia, recent series have aired nationally on Foxtel within a few hours of their UK release. Series 1–6 were broadcast on ABC One a few months behind original broadcast in the U.K. Generally, this was shown in a 7:30pm Saturday timeslot.
In Canada, all series have been broadcast on BBC Canada on Thursdays at 9:00 pm. The last two series have been shown about a month after the BBC One showing.
In Latvia, the programme is broadcast on Latvian Television from Monday to Thursday at 6:55 pm, started airing with series 3 in 2018.[46]
Music[edit]
Theme music[edit]
The theme music is an instrumental version of a Jamaican song from the 1960s, "You're Wondering Now," written by Coxsone Dodd, originally recorded by Andy & Joey in Jamaica. It was later made famous by The Skatalites and in Europe by ska band The Specials and later still by Amy Winehouse as featured on some editions of the deluxe version of her album Back to Black. In the first episode of the third series, the cover version recorded by The Skatalites in 1994 is played at the bar. It appeared on the official Death in Paradise soundtrack, released in January 2015, alongside other music from all four series. In the French version, the opening song is "Sunday Shining" by Finley Quaye.
Soundtrack[edit]
In January 2015, an official soundtrack compiling 26 songs from the first four series of the show was released by the BBC. It contains original music for Death in Paradise and already extant tunes, though it does not include the theme music from the show.
Novels[edit]
The creator of the show, Robert Thorogood, signed a three-book deal to write Death in Paradise novels featuring the original characters (D.I. Richard Poole, D.S. Camille Bordey, Officer Dwayne Myers, Sergeant Fidel Best and Comm. Selwyn Patterson). The first of these, A Meditation on Murder (A Death in Paradise novel),[47] was published in January 2015. Early reviews were generally favourable, with the Daily Express in particular being complimentary, giving it four stars.[48] The second book was released in 2016 with the title The Killing of Polly Carter. The third book, titled Death Knocks Twice was released in 2017. An additional fourth book, Murder in the Caribbean, is due to be released late 2018.
Notes[edit]
Jump up ^ Series 4, episode 7 was shown in an earlier timeslot of 8.25 pm-9.25 pm due to EastEnders Live 30th anniversary celebrations.
References[edit]
Jump up ^ "Death in Paradise series three confirmed". Radio Times. Retrieved 12 February 2013.
Jump up ^ Plunkett, John (27 February 2014). "David Walliams to star as BBC bags Agatha Christie drama deal". The Guardian. Retrieved 25 October 2014.
Jump up ^ "BBC – Ardal O'Hanlon set for Paradise – Media Centre". www.bbc.co.uk. Retrieved 17 February 2017.
Jump up ^ "Death in Paradise will return with Ardal O'Hanlon". 1 February 2018.
Jump up ^ "BBC One – Death in Paradise". bbc.co.uk. 26 February 2015. Retrieved 30 March 2015.
Jump up ^ "About Series 1 | Death in Paradise | Alibi Channel". Alibi.uktv.co.uk. Retrieved 30 March 2015.
Jump up ^ "Weekly Top 30 Programmes (see relevant week(s))". BARB.
Jump up ^ Jack Seale. "What is the Secret to Death in Paradise?" The Guardian, 19 February 2015. [1].
Jump up ^ "Death In Paradise did have its quirks but it was too formulaic and a touch lazy 4 Mar 2014". Metro. Retrieved 14 December 2016.
Jump up ^ "The secrets of Death in Paradise 7 January 2016". Radio Times. Retrieved 14 December 2016.
Jump up ^ "Success in Paradise!!!! 28 February 2015". Amazon. Retrieved 14 December 2016.
Jump up ^ "Death in Paradise: how on earth does this get so many viewers? 12 February 2013". The Guardian. Retrieved 14 December 2016.
Jump up ^ "Harmless Nonsense, Nice Palm Trees, 10 April 2015". Amazon. Retrieved 14 December 2016.
Jump up ^ "Episode 5, Series 5, Death in Paradise – BBC One". Retrieved 20 July 2016.
Jump up ^ "Episode 6, Series 5, Death in Paradise – BBC One". Retrieved 20 July 2016.
Jump up ^ "Death in Paradise axes longtime star Danny John Jules as Dwayne".
Jump up ^ "How, when and why is Danny John-Jules leaving Death in Paradise?". Retrieved 21 June 2018.
Jump up ^ "Meurtre au paradis. L'industrie du cinéma teste la Guadeloupe – Abonnement". Guadeloupe.franceantilles.fr. 16 September 2011. Retrieved 30 March 2015.
Jump up ^ Skinitis, Alexia (2017-01-05). "Where is Death in Paradise filmed? Guadeloupe location guide". Radiotimes.com. Retrieved 2017-02-24.
Jump up ^ "Kris Marshall swaps Death In Paradise for family time - BBC News". Bbc.co.uk. 2017-02-02. Retrieved 2017-02-24.
Jump up ^ "BBC One - Death in Paradise, Series 6, Episode 7". Bbc.co.uk. 2017-02-16. Retrieved 2017-02-24.
Jump up ^ "Weekly top 30 programmes - BARB". www.barb.co.uk.
Jump up ^ "Death in Paradise, episode one, review". Telegraph. Retrieved 30 March 2015.
Jump up ^ "Death in Paradise, series 4, episode 2, review". Telegraph. Retrieved 30 March 2015.
Jump up ^ "Red Planet Pictures". Retrieved 27 February 2015.
Jump up ^ "Death in Paradise – Series 1 (DVD)". BBCShop.com. Retrieved 21 May 2012.
Jump up ^ "Death in Paradise: Series 1: Ben Miller, Sara Martins, Danny John-Jules, Various: Movies & TV". Amazon.com. Retrieved 30 March 2015.
Jump up ^ "Death In Paradise - Series 1". www.jbhifi.com.au.
Jump up ^ "Death in Paradise: Season 2: Ben Miller, Sara Martins, Danny John-Jules, Gary Carr, Elizabeth Bourgine, Various: Movies & TV". Amazon.com. Retrieved 30 March 2015.
Jump up ^ "Death In Paradise - Series 2". www.jbhifi.com.au.
Jump up ^ "Death in Paradise: Series 3 (DVD): Various: Movies & TV". Amazon.com. Retrieved 30 March 2015.
Jump up ^ "Death In Paradise - Series 3". www.jbhifi.com.au.
Jump up ^ "Death in Paradise – Series 4 [DVD] [2015]: Amazon.co.uk: Kris Marshall: DVD & Blu-ray". Amazon.co.uk. Retrieved 30 March 2015.
Jump up ^ "Death in Paradise: Series 4 (DVD): Various: Movies & TV". Amazon.com. Retrieved 5 May 2018.
Jump up ^ "Death In Paradise - Series 4". www.jbhifi.com.au.
Jump up ^ "Death in Paradise: Series 5 (DVD): Various: Movies & TV". Amazon.com. Retrieved 5 May 2018.
Jump up ^ "Death In Paradise - Series 5". www.jbhifi.com.au.
Jump up ^ "Death In Paradise - Series 1-5". www.jbhifi.com.au.
Jump up ^ "Death in Paradise: Series 6 (DVD): Various: Movies & TV". Amazon.com. Retrieved 5 May 2018.
Jump up ^ "Death In Paradise: Series 6". www.jbhifi.com.au.
Jump up ^ "Death In Paradise: Series 1-6". www.jbhifi.com.au.
Jump up ^ "Buy Death in Paradise: Series 7 on DVD from EzyDVD.com.au". www.ezydvd.com.au.
Jump up ^ "Buy Death in Paradise: Series 1 - 7 on DVD from EzyDVD.com.au". www.ezydvd.com.au.
Jump up ^ "Death In Paradise | KQED Public Media for Northern CA". Kqed.org. Retrieved 30 March 2015.
Jump up ^ KBTC.org; Programming@KBTC.org; KBTC Public Television PBS, 2320 South 19th Street, Tacoma, WA 98405.
Jump up ^ "Detektīvseriāls. «Nāve paradīzē» 1. - 4. sērija" (in Latvian). ltv.lsm.lv. 25 June 2018. Retrieved 17 July 2018.
Jump up ^ "A Meditation on Murder (An original Death in Paradise story): Amazon.co.uk: Robert Thorogood: 8601410743390: Books". Amazon.co.uk. Retrieved 30 March 2015.
Jump up ^ Coates, Jon (30 January 2015). "Book reviews: January's crime and detective fiction investigated". Daily Express. Northern & Shell. Retrieved 30 March 2015.
All ratings are sourced from the Broadcasters' Audience Research Board (BARB).
External links[edit]
Death in Paradise at BBC Programmes
Death in Paradise at epguides.com
Death in Paradise on IMDb
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Wind wave
From Wikipedia, the free encyclopedia
Jump to navigation Jump to search
"Ocean wave" redirects here. For the film, see Ocean Waves (film).
Large wave
Play media
Video of large waves from Hurricane Marie along the coast of Newport Beach, California
Ocean waves
In fluid dynamics, wind waves, or wind-generated waves, are surface waves that occur on the free surface of bodies of water (like oceans, seas, lakes, rivers, canals, puddles or ponds). They result from the wind blowing over an area of fluid surface. Waves in the oceans can travel thousands of miles before reaching land. Wind waves on Earth range in size from small ripples, to waves over 100 ft (30 m) high.[1]
When directly generated and affected by local winds, a wind wave system is called a wind sea. After the wind ceases to blow, wind waves are called swells. More generally, a swell consists of wind-generated waves that are not significantly affected by the local wind at that time. They have been generated elsewhere or some time ago.[2] Wind waves in the ocean are called ocean surface waves.
Wind waves have a certain amount of randomness: subsequent waves differ in height, duration, and shape with limited predictability. They can be described as a stochastic process, in combination with the physics governing their generation, growth, propagation, and decay—as well as governing the interdependence between flow quantities such as: the water surface movements, flow velocities and water pressure. The key statistics of wind waves (both seas and swells) in evolving sea states can be predicted with wind wave models.
Although waves are usually considered in the water seas of Earth, the hydrocarbon seas of Titan may also have wind-driven waves.[3]
Contents
1 Wave formation
2 Types of wind waves
3 Wave shoaling and refraction
4 Wave breaking
5 Physics of waves
6 Wind wave models
7 Seismic signals
8 Internal waves
9 See also
10 Notes
11 References
11.1 Scientific
11.2 Other
12 External links
Wave formation[edit]
Aspects of a water wave
Wave formation
Water particle motion of a deep water wave
The phases of an ocean surface wave: 1. Wave Crest, where the water masses of the surface layer are moving horizontally in the same direction as the propagating wave front. 2. Falling wave. 3. Trough, where the water masses of the surface layer are moving horizontally in the opposite direction of the wave front direction. 4. Rising wave.
NOAA ship Delaware II in bad weather on Georges Bank
The great majority of large breakers seen at a beach result from distant winds. Five factors influence the formation of the flow structures in wind waves:[4]
Wind speed or strength relative to wave speed—the wind must be moving faster than the wave crest for energy transfer
The uninterrupted distance of open water over which the wind blows without significant change in direction (called the fetch)
Width of area affected by fetch[clarification needed]
Wind duration — the time for which the wind has blown over the water.
Water depth
All of these factors work together to determine the size of wind waves and the structure of the flow within them.
The main dimensions associated with waves are:
Wave height (vertical distance from trough to crest)
Wave length (distance from crest to crest in the direction of propagation)
Wave period (time interval between arrival of consecutive crests at a stationary point)
Wave propagation direction
A fully developed sea has the maximum wave size theoretically possible for a wind of a specific strength, duration, and fetch. Further exposure to that specific wind could only cause a dissipation of energy due to the breaking of wave tops and formation of "whitecaps". Waves in a given area typically have a range of heights. For weather reporting and for scientific analysis of wind wave statistics, their characteristic height over a period of time is usually expressed as significant wave height. This figure represents an average height of the highest one-third of the waves in a given time period (usually chosen somewhere in the range from 20 minutes to twelve hours), or in a specific wave or storm system. The significant wave height is also the value a "trained observer" (e.g. from a ship's crew) would estimate from visual observation of a sea state. Given the variability of wave height, the largest individual waves are likely to be somewhat less than twice the reported significant wave height for a particular day or storm.[5]
Wave formation on an initially flat water surface by wind is started by a random distribution of normal pressure of turbulent wind flow over the water. This pressure fluctuation produces normal and tangential stresses in the surface water, which generates waves. It is assumed that:[6]
The water is originally at rest.
The water is not viscous.
The water is irrotational.
There is a random distribution of normal pressure to the water surface from the turbulent wind.
Correlations between air and water motions are neglected.
The second mechanism involves wind shear forces on the water surface. John W. Miles suggested a surface wave generation mechanism which is initiated by turbulent wind shear flows based on the inviscid Orr-Sommerfeld equation in 1957. He found the energy transfer from wind to water surface is proportional to the curvature of the velocity profile of the wind at the point where the mean wind speed is equal to the wave speed. Since the wind speed profile is logarithmic to the water surface, the curvature has a negative sign at this point. This relation shows the wind flow transferring its kinetic energy to the water surface at their interface.
Assumptions:
two-dimensional parallel shear flow
incompressible, inviscid water and wind
irrotational water
slope of the displacement of the water surface is small[7]
Generally these wave formation mechanisms occur together on the water surface and eventually produce fully developed waves.
For example,[8] if we assume a flat sea surface (Beaufort state 0), and a sudden wind flow blows steadily across the sea surface, the physical wave generation process follows the sequence:
Turbulent wind forms random pressure fluctuations at the sea surface. Ripples with wavelengths in the order of a few centimetres are generated by the pressure fluctuations. (The Phillips mechanism[6])
The winds keep acting on the initially rippled sea surface causing the waves to become larger. As the waves grow, the pressure differences get larger causing the growth rate to increase. Finally the shear instability expedites the wave growth exponentially. (The Miles mechanism[6])
The interactions between the waves on the surface generate longer waves[9] and the interaction will transfer wave energy from the shorter waves generated by the Miles mechanism to the waves which have slightly lower frequencies than the frequency at the peak wave magnitudes, then finally the waves will be faster than the cross wind speed (Pierson & Moskowitz[10]).
hideConditions necessary for a fully developed sea at given wind speeds, and the parameters of the resulting waves
Wind conditions
Wave size
Wind speed in one direction
Fetch
Wind duration
Average height
Average wavelength
Average period and speed
19 km/h (12 mph) 19 km (12 mi) 2 hr 0.27 m (0.89 ft) 8.5 m (28 ft) 3.0 sec, 10.2 km/h (9.3 ft/sec)
37 km/h (23 mph) 139 km (86 mi) 10 hr 1.5 m (4.9 ft) 33.8 m (111 ft) 5.7 sec, 21.4 km/h (19.5 ft/sec)
56 km/h (35 mph) 518 km (322 mi) 23 hr 4.1 m (13 ft) 76.5 m (251 ft) 8.6 sec, 32.0 km/h (29.2 ft/sec)
74 km/h (46 mph) 1,313 km (816 mi) 42 hr 8.5 m (28 ft) 136 m (446 ft) 11.4 sec, 42.9 km/h (39.1 ft/sec)
92 km/h (57 mph) 2,627 km (1,632 mi) 69 hr 14.8 m (49 ft) 212.2 m (696 ft) 14.3 sec, 53.4 km/h (48.7 ft/sec)
NOTE: Most of the wave speeds calculated from the wave length divided by the period are proportional to the square root of the wave length. Thus, except for the shortest wave length, the waves follow the deep water theory. The 28 ft long wave must be either in shallow water or intermediate depth.
Types of wind waves[edit]
Classification of the spectrum of ocean waves according to wave period[11]
Surf on a rocky irregular bottom. Porto Covo, west coast of Portugal
Three different types of wind waves develop over time:
Capillary waves, or ripples
Seas
Swells
Ripples appear on smooth water when the wind blows, but will die quickly if the wind stops. The restoring force that allows them to propagate is surface tension. Sea waves are larger-scale, often irregular motions that form under sustained winds. These waves tend to last much longer, even after the wind has died, and the restoring force that allows them to propagate is gravity. As waves propagate away from their area of origin, they naturally separate into groups of common direction and wavelength. The sets of waves formed in this manner are known as swells.
Individual "rogue waves" (also called "freak waves", "monster waves", "killer waves", and "king waves") much higher than the other waves in the sea state can occur. In the case of the Draupner wave, its 25 m (82 ft) height was 2.2 times the significant wave height. Such waves are distinct from tides, caused by the Moon and Sun's gravitational pull, tsunamis that are caused by underwater earthquakes or landslides, and waves generated by underwater explosions or the fall of meteorites—all having far longer wavelengths than wind waves.
Yet, the largest ever recorded wind waves are common — not rogue — waves in extreme sea states. For example: 29.1 m (95 ft) high waves have been recorded on the RRS Discovery in a sea with 18.5 m (61 ft) significant wave height, so the highest wave is only 1.6 times the significant wave height.[12] The biggest recorded by a buoy (as of 2011) was 32.3 m (106 ft) high during the 2007 typhoon Krosa near Taiwan.[13]
Ocean waves can be classified based on: the disturbing force(s) that create(s) them; the extent to which the disturbing force(s) continue(s) to influence them after formation; the extent to which the restoring force(s) weaken(s) (or flatten) them; and their wavelength or period. Seismic Sea waves have a period of ~20 minutes, and speeds of 760 km/h (470 mph). Wind waves (deep-water waves) have a period of about 20 seconds.
[14]
Wave type
Typical wavelength
Disturbing force
Restoring force
Capillary wave < 2 cm Wind Surface tension
Wind wave 60–150 m (200–490 ft) Wind over ocean Gravity
Seiche Large, variable; a function of basin size Change in atmospheric pressure, storm surge Gravity
Seismic sea wave (tsunami) 200 km (120 mi) Faulting of sea floor, volcanic eruption, landslide Gravity
Tide Half the circumference of Earth Gravitational attraction, rotation of Earth Gravity
The speed of all ocean waves is controlled by gravity, wavelength, and water depth. Most characteristics of ocean waves depend on the relationship between their wavelength and water depth. Wavelength determines the size of the orbits of water molecules within a wave, but water depth determines the shape of the orbits. The paths of water molecules in a wind wave are circular only when the wave is traveling in deep water. A wave cannot "feel" the bottom when it moves through water deeper than half its wavelength because too little wave energy is contained in the small circles below that depth. Waves moving through water deeper than half their wavelength are known as deep-water waves. On the other hand, the orbits of water molecules in waves moving through shallow water are flattened by the proximity of the sea surface bottom. Waves in water shallower than 1/20 their original wavelength are known as shallow-water waves. Transitional waves travel through water deeper than 1/20 their original wavelength but shallower than half their original wavelength.
In general, the longer the wavelength, the faster the wave energy will move through the water. For deep-water waves, this relationship is represented with the following formula:
C = L / T {\displaystyle C={L}/{T}}
where C is speed (celerity), L is wavelength, and T is time, or period (in seconds).
The speed of a deep-water wave may also be approximated by:
C = g L / 2 π {\displaystyle C={\sqrt {{gL}/{2\pi }}}}
where g is the acceleration due to gravity, 9.8 meters (32 feet) per second squared. Because g and π (3.14) are constants, the equation can be reduced to:
C = 1.251 L {\displaystyle C=1.251{\sqrt {L}}}
when C is measured in meters per second and L in meters. Note that in both formulas the wave speed is proportional to the square root of the wavelength.
The speed of shallow-water waves is described by a different equation that may be written as:
C = g d = 3.1 d {\displaystyle C={\sqrt {gd}}=3.1{\sqrt {d}}}
where C is speed (in meters per second), g is the acceleration due to gravity, and d is the depth of the water (in meters). The period of a wave remains unchanged regardless of the depth of water through which it is moving. As deep-water waves enter the shallows and feel the bottom, however, their speed is reduced and their crests "bunch up," so their wavelength shortens.
Wave shoaling and refraction[edit]
See also: wave shoaling and refraction
As waves travel from deep to shallow water, their shape alters (wave height increases, speed decreases, and length decreases as wave orbits become asymmetrical). This process is called shoaling.
Wave refraction is the process that occurs when waves interact with the sea bed as the wave crests align themselves as a result of approaching decreasing water depths at an angle to the depth contours. Varying depths along a wave crest cause the crest to travel at different phase speeds, with those parts of the wave in deeper water moving faster than those in shallow water. This process continues until the crests become (nearly) parallel to the depth contours. Rays—lines normal to wave crests between which a fixed amount of energy flux is contained—converge on local shallows and shoals. Therefore, the wave energy between rays is concentrated as they converge, with a resulting increase in wave height.
Because these effects are related to a spatial variation in the phase speed, and because the phase speed also changes with the ambient current – due to the Doppler shift – the same effects of refraction and altering wave height also occur due to current variations. In the case of meeting an adverse current the wave steepens, i.e. its wave height increases while the wave length decreases, similar to the shoaling when the water depth decreases.[15]
Wave breaking[edit]
Big wave breaking
See also: surf wave, breaking wave, and Iribarren number
Some waves undergo a phenomenon called "breaking".[16] A breaking wave is one whose base can no longer support its top, causing it to collapse. A wave breaks when it runs into shallow water, or when two wave systems oppose and combine forces. When the slope, or steepness ratio, of a wave is too great, breaking is inevitable.
Individual waves in deep water break when the wave steepness—the ratio of the wave height H to the wavelength λ—exceeds about 0.17, so for H > 0.17 λ. In shallow water, with the water depth small compared to the wavelength, the individual waves break when their wave height H is larger than 0.8 times the water depth h, that is H > 0.8 h.[17] Waves can also break if the wind grows strong enough to blow the crest off the base of the wave.
In shallow water the base of the wave is decelerated by drag on the seabed. As a result, the upper parts will propagate at a higher velocity than the base and the leading face of the crest will become steeper and the trailing face flatter. This may be exaggerated to the extent that the leading face forms a barrel profile, with the crest falling forward and down as it extends over the air ahead of the wave.
Three main types of breaking waves are identified by surfers or surf lifesavers. Their varying characteristics make them more or less suitable for surfing, and present different dangers.
Spilling, or rolling: these are the safest waves on which to surf. They can be found in most areas with relatively flat shorelines. They are the most common type of shorebreak. The deceleration of the wave base is gradual, and the velocity of the upper parts does not differ much with height. Breaking occurs mainly when the steepness ratio exceeds the stability limit.
Plunging, or dumping: these break suddenly and can "dump" swimmers—pushing them to the bottom with great force. These are the preferred waves for experienced surfers. Strong offshore winds and long wave periods can cause dumpers. They are often found where there is a sudden rise in the sea floor, such as a reef or sandbar. Deceleration of the wave base is sufficient to cause upward acceleration and a significant forward velocity excess of the upper part of the crest. The peak rises and overtakes the forward face, forming a "barrel" or "tube" as it collapses.
Surging: these may never actually break as they approach the water's edge, as the water below them is very deep. They tend to form on steep shorelines. These waves can knock swimmers over and drag them back into deeper water.
When the shoreline is near vertical, waves do not break, but are reflected. Most of the energy is retained in the wave as it returns to seaward. Interference patterns are caused by superposition of the incident and reflected waves, and the superposition may cause localised instability when peaks cross, and these peaks may break due to instability. (see also clapotic waves)
Physics of waves[edit]
See also: Airy wave theory
Stokes drift in shallow water waves (Animation)
Wind waves are mechanical waves that propagate along the interface between water and air; the restoring force is provided by gravity, and so they are often referred to as surface gravity waves. As the wind blows, pressure and friction perturb the equilibrium of the water surface and transfer energy from the air to the water, forming waves. The initial formation of waves by the wind is described in the theory of Phillips from 1957, and the subsequent growth of the small waves has been modeled by Miles, also in 1957.[18][19]
Stokes drift in a deeper water wave (Animation)
Photograph of the water particle orbits under a – progressive and periodic – surface gravity wave in a wave flume. The wave conditions are: mean water depth d = 2.50 ft (0.76 m), wave height H = 0.339 ft (0.103 m), wavelength λ = 6.42 ft (1.96 m), period T = 1.12 s.[20]
In linear plane waves of one wavelength in deep water, parcels near the surface move not plainly up and down but in circular orbits: forward above and backward below (compared the wave propagation direction). As a result, the surface of the water forms not an exact sine wave, but more a trochoid with the sharper curves upwards—as modeled in trochoidal wave theory. Wind waves are thus a combination of transversal and longitudinal waves.
When waves propagate in shallow water, (where the depth is less than half the wavelength) the particle trajectories are compressed into ellipses.[21][22]
In reality, for finite values of the wave amplitude (height), the particle paths do not form closed orbits; rather, after the passage of each crest, particles are displaced slightly from their previous positions, a phenomenon known as Stokes drift.[23][24]
As the depth below the free surface increases, the radius of the circular motion decreases. At a depth equal to half the wavelength λ, the orbital movement has decayed to less than 5% of its value at the surface. The phase speed (also called the celerity) of a surface gravity wave is – for pure periodic wave motion of small-amplitude waves – well approximated by
c = g λ 2 π tanh  ( 2 π d λ ) {\displaystyle c={\sqrt {{\frac {g\lambda }{2\pi }}\tanh \left({\frac {2\pi d}{\lambda }}\right)}}}
where
c = phase speed;
λ = wavelength;
d = water depth;
g = acceleration due to gravity at the Earth's surface.
In deep water, where d ≥ 1 2 λ {\displaystyle d\geq {\frac {1}{2}}\lambda } , so 2 π d λ ≥ π {\displaystyle {\frac {2\pi d}{\lambda }}\geq \pi } and the hyperbolic tangent approaches 1 {\displaystyle 1} , the speed c {\displaystyle c} approximates
c deep = g λ 2 π . {\displaystyle c_{\text{deep}}={\sqrt {\frac {g\lambda }{2\pi }}}.}
In SI units, with c deep {\displaystyle c_{\text{deep}}} in m/s, c deep ≈ 1.25 λ {\displaystyle c_{\text{deep}}\approx 1.25{\sqrt {\lambda }}} , when λ {\displaystyle \lambda } is measured in metres. This expression tells us that waves of different wavelengths travel at different speeds. The fastest waves in a storm are the ones with the longest wavelength. As a result, after a storm, the first waves to arrive on the coast are the long-wavelength swells.
For intermediate and shallow water, the Boussinesq equations are applicable, combining frequency dispersion and nonlinear effects. And in very shallow water, the shallow water equations can be used.
If the wavelength is very long compared to the water depth, the phase speed (by taking the limit of c when the wavelength approaches infinity) can be approximated by
c shallow = lim λ → ∞ c = g d . {\displaystyle c_{\text{shallow}}=\lim _{\lambda \rightarrow \infty }c={\sqrt {gd}}.}
On the other hand, for very short wavelengths, surface tension plays an important role and the phase speed of these gravity-capillary waves can (in deep water) be approximated by
c gravity-capillary = g λ 2 π + 2 π S ρ λ {\displaystyle c_{\text{gravity-capillary}}={\sqrt {{\frac {g\lambda }{2\pi }}+{\frac {2\pi S}{\rho \lambda }}}}}
where
S = surface tension of the air-water interface;
ρ {\displaystyle \rho } = density of the water.[25]
When several wave trains are present, as is always the case in nature, the waves form groups. In deep water the groups travel at a group velocity which is half of the phase speed.[26] Following a single wave in a group one can see the wave appearing at the back of the group, growing and finally disappearing at the front of the group.
As the water depth d {\displaystyle d} decreases towards the coast, this will have an effect: wave height changes due to wave shoaling and refraction. As the wave height increases, the wave may become unstable when the crest of the wave moves faster than the trough. This causes surf, a breaking of the waves.
The movement of wind waves can be captured by wave energy devices. The energy density (per unit area) of regular sinusoidal waves depends on the water density ρ {\displaystyle \rho } , gravity acceleration g {\displaystyle g} and the wave height H {\displaystyle H} (which, for regular waves, is equal to twice the amplitude, a {\displaystyle a} ):
E = 1 8 ρ g H 2 = 1 2 ρ g a 2 . {\displaystyle E={\frac {1}{8}}\rho gH^{2}={\frac {1}{2}}\rho ga^{2}.}
The velocity of propagation of this energy is the group velocity.
Wind wave models[edit]
The image shows the global distribution of wind speed and wave height as observed by NASA's TOPEX/Poseidon's dual-frequency radar altimeter from October 3 to October 12, 1992. Simultaneous observations of wind speed and wave height are helping scientists to predict ocean waves. Wind speed is determined by the strength of the radar signal after it has bounced off the ocean surface and returned to the satellite. A calm sea serves as a good reflector and returns a strong signal; a rough sea tends to scatter the signals and returns a weak pulse. Wave height is determined by the shape of the return radar pulse. A calm sea with low waves returns a condensed pulse whereas a rough sea with high waves returns a stretched pulse. Comparing the two images above shows a high degree of correlation between wind speed and wave height. The strongest winds (33.6 mph; 54.1 km/h) and highest waves are found in the Southern Ocean. The weakest winds — shown as areas of magenta and dark blue — are generally found in the tropical oceans.
Main article: Wind wave model
Surfers are very interested in the wave forecasts. There are many websites that provide predictions of the surf quality for the upcoming days and weeks. Wind wave models are driven by more general weather models that predict the winds and pressures over the oceans, seas and lakes.
Wind wave models are also an important part of examining the impact of shore protection and beach nourishment proposals. For many beach areas there is only patchy information about the wave climate, therefore estimating the effect of wind waves is important for managing littoral environments.
Seismic signals[edit]
Main article: microseism
Ocean water waves generate land seismic waves that propagate hundreds of kilometers into the land.[27] These seismic signals usually have the period of 6 ± 2 seconds. Such recordings were first reported and understood in about 1900.
There are two types of seismic "ocean waves". The primary waves are generated in shallow waters by direct water wave-land interaction and have the same period as the water waves (10 to 16 seconds). The more powerful secondary waves are generated by the superposition of ocean waves of equal period traveling in opposite directions, thus generating standing gravity waves – with an associated pressure oscillation at half the period, which is not diminishing with depth. The theory for microseism generation by standing waves was provided by Michael Longuet-Higgins in 1950, after in 1941 Pierre Bernard suggested this relation with standing waves on the basis of observations.[28][29]
Internal waves[edit]
Main article: Internal wave
See also[edit]
Airy wave theory
Breakwater (structure)
Boussinesq approximation (water waves)
Clapotis
Cross sea
Gravity wave
Luke's variational principle
Mild-slope equation
Rogue wave
Shallow water equations
Tsunami
Wave power
Wave radar
Waves and shallow water
Notes[edit]
Jump up ^ Tolman, H. L. (23 June 2010). Mahmood, M.F., ed. "CBMS Conference Proceedings on Water Waves: Theory and Experiment" (PDF). Howard University, US, 13–18 May 2008: World Scientific Publications. ISBN 978-981-4304-23-8.
Jump up ^ Holthuijsen (2007), page 5.
Jump up ^ Lorenz, R. D.; Hayes, A. G. (2012). "The Growth of Wind-Waves in Titan's Hydrocarbon Seas". Icarus. 219: 468–475. Bibcode:2012Icar..219..468L. doi:10.1016/j.icarus.2012.03.002.
Jump up ^ Young, I. R. (1999). Wind generated ocean waves. Elsevier. p. 83. ISBN 0-08-043317-0.
Jump up ^ Weisse, Ralf; von Storch, Hans (2008). Marine climate change: Ocean waves, storms and surges in the perspective of climate change. Springer. p. 51. ISBN 978-3-540-25316-7.
^ Jump up to: a b c Phillips, O. M. (2006). "On the generation of waves by turbulent wind". Journal of Fluid Mechanics. 2 (5): 417. Bibcode:1957JFM.....2..417P. doi:10.1017/S0022112057000233.
Jump up ^ Miles, John W. (2006). "On the generation of surface waves by shear flows". Journal of Fluid Mechanics. 3 (2): 185. Bibcode:1957JFM.....3..185M. doi:10.1017/S0022112057000567.
Jump up ^ Chapter 16, Ocean Waves
Jump up ^ Hasselmann, K.; et al. (1973). "Measurements of wind-wave growth and swell decay during the Joint North Sea Wave Project (JONSWAP)". Ergnzungsheft zur Deutschen Hydrographischen Zeitschrift Reihe A. 8 (12): 95. hdl:10013/epic.20654.
Jump up ^ Pierson, Willard J.; Moskowitz, Lionel (15 December 1964). "A proposed spectral form for fully developed wind seas based on the similarity theory of S. A. Kitaigorodskii". Journal of Geophysical Research. 69 (24): 5181–5190. Bibcode:1964JGR....69.5181P. doi:10.1029/JZ069i024p05181.
Jump up ^ Munk, Walter H. (1950). "Proceedings 1st International Conference on Coastal Engineering". Long Beach, California: ASCE: 1–4.
Jump up ^ Holliday, Naomi P.; Yelland, Margaret J.; Pascal, Robin; Swail, Val R.; Taylor, Peter K.; Griffiths, Colin R.; Kent, Elizabeth (2006). "Were extreme waves in the Rockall Trough the largest ever recorded?". Geophysical Research Letters. 33 (L05613). Bibcode:2006GeoRL..3305613H. doi:10.1029/2005GL025238.
Jump up ^ P. C. Liu; H. S. Chen; D.-J. Doong; C. C. Kao; Y.-J. G. Hsu (11 June 2008). "Monstrous ocean waves during typhoon Krosa" (PDF). Annales Geophysicae. European Geosciences Union. 26 (6): 1327–1329. Bibcode:2008AnGeo..26.1327L. doi:10.5194/angeo-26-1327-2008.
Jump up ^ Tom Garrison (2009). Oceanography: An Invitation to Marine Science (7th Edition). Yolanda Cossio. ISBN 978-0495391937.
Jump up ^ Longuet-Higgins, M. S.; Stewart, R. W. (1964). "Radiation stresses in water waves; a physical discussion, with applications". Deep-Sea Research. 11 (4): 529–562. Bibcode:1964DSROA..11..529L. doi:10.1016/0011-7471(64)90001-4.
Jump up ^ Gulrez, Tauseef; Hassanien, Aboul Ella (2011-11-13). Advances in Robotics and Virtual Reality. Springer Science & Business Media. ISBN 9783642233630.
Jump up ^ R.J. Dean and R.A. Dalrymple (2002). Coastal processes with engineering applications. Cambridge University Press. ISBN 0-521-60275-0. p. 96–97.
Jump up ^ Phillips, O. M. (1957). "On the generation of waves by turbulent wind". Journal of Fluid Mechanics. 2 (5): 417–445. Bibcode:1957JFM.....2..417P. doi:10.1017/S0022112057000233.
Jump up ^ Miles, J. W. (1957). "On the generation of surface waves by shear flows". Journal of Fluid Mechanics. 3 (2): 185–204. Bibcode:1957JFM.....3..185M. doi:10.1017/S0022112057000567.
Jump up ^ Figure 6 from: Wiegel, R. L.; Johnson, J. W. (1950). "Proceedings 1st International Conference on Coastal Engineering". Long Beach, California: ASCE: 5–21.
Jump up ^ For the particle trajectories within the framework of linear wave theory, see for instance:
Phillips (1977), page 44.
Lamb, H. (1994). Hydrodynamics (6th ed.). Cambridge University Press. ISBN 978-0-521-45868-9. Originally published in 1879, the 6th extended edition appeared first in 1932. See §229, page 367.
L. D. Landau and E. M. Lifshitz (1986). Fluid mechanics. Course of Theoretical Physics. 6 (Second revised ed.). Pergamon Press. ISBN 0-08-033932-8. See page 33.
Jump up ^ A good illustration of the wave motion according to linear theory is given by Prof. Robert Dalrymple's Java applet.
Jump up ^ For nonlinear waves, the particle paths are not closed, as found by George Gabriel Stokes in 1847, see the original paper by Stokes. Or in Phillips (1977), page 44: "To this order, it is evident that the particle paths are not exactly closed ... pointed out by Stokes (1847) in his classical investigation".
Jump up ^ Solutions of the particle trajectories in fully nonlinear periodic waves and the Lagrangian wave period they experience can for instance be found in:
J. M. Williams (1981). "Limiting gravity waves in water of finite depth". Philosophical Transactions of the Royal Society A. 302 (1466): 139–188. Bibcode:1981RSPTA.302..139W. doi:10.1098/rsta.1981.0159.
J. M. Williams (1985). Tables of progressive gravity waves. Pitman. ISBN 978-0-273-08733-5.
Jump up ^ Carl Nordling, Jonny Östermalm (2006). Physics Handbook for Science and Engineering (Eight ed.). Studentliteratur. p. 263. ISBN 978-91-44-04453-8.
Jump up ^ In deep water, the group velocity is half the phase velocity, as is shown here. Another reference is [1].
Jump up ^ Peter Bormann. Seismic Signals and Noise
Jump up ^ Bernard, P. (1941). "Sur certaines proprietes de la boule etudiees a l'aide des enregistrements seismographiques". Bulletin de l'Institut océanographique de Monaco. 800: 1–19.
Jump up ^ Longuet-Higgins, M. S. (1950). "A theory of the origin of microseisms". Philosophical Transactions of the Royal Society A. 243 (857): 1–35. Bibcode:1950RSPTA.243....1L. doi:10.1098/rsta.1950.0012.
References[edit]
Scientific[edit]
G. G. Stokes (1880). Mathematical and Physical Papers, Volume I. Cambridge University Press. pp. 197–229.
Phillips, O. M. (1977). The dynamics of the upper ocean (2nd ed.). Cambridge University Press. ISBN 0-521-29801-6.
Holthuijsen, Leo H. (2007). Waves in oceanic and coastal waters. Cambridge University Press. ISBN 0-521-86028-8.
Janssen, Peter (2004). The interaction of ocean waves and wind. Cambridge University Press. ISBN 978-0-521-46540-3.
Other[edit]
Rousmaniere, John (1989). The Annapolis Book of Seamanship (2nd revised ed.). Simon & Schuster. ISBN 0-671-67447-1.
Carr, Michael (October 1998). "Understanding Waves". Sail. pp. 38–45.
External links[edit]
Wikiquote has quotations related to: Wind wave
Wikimedia Commons has media related to Ocean surface waves.
Wikimedia Commons has media related to Water waves.
"Anatomy of a Wave" Holben, Jay boatsafe.com captured 5/23/06
NOAA National Weather Service
ESA press release on swell tracking with ASAR onboard ENVISAT
Introductory oceanography chapter 10 – Ocean Waves
HyperPhysics – Ocean Waves
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Wave period

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/wiki/Period_(physics)
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Period (physics)

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values: {\displaystyle C={\sqrt {{gL}/{2\pi }}}}

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values: {\displaystyle C={\sqrt {gd}}=3.1{\sqrt {d}}}

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Phase speed

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Waves in shallow water

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Wave energy

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Doppler shift

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Surface gravity wave

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Transversal wave

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values: c=\sqrt{\frac{g \lambda}{2\pi} \tanh \left(\frac{2\pi d}{\lambda}\right)}

values: {\displaystyle d\geq {\frac {1}{2}}\lambda }

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values: {\displaystyle {\frac {2\pi d}{\lambda }}\geq \pi }

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values: c_\text{shallow} = \lim_{\lambda\rightarrow\infty} c = \sqrt{gd}.

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/wiki/Gravity-capillary_wave
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Gravity-capillary wave

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values: c_\text{gravity-capillary}=\sqrt{\frac{g \lambda}{2\pi} + \frac{2\pi S}{\rho\lambda}}

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Trough (physics)

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Coastal protection

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Billabong Pro Jeffreys Bay

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