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Saturday Night Live cast members
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For information on the cast lineup as of September 2017, see Saturday Night Live (season 43).
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The original cast (l to r): Laraine Newman, John Belushi, Jane Curtin, Gilda Radner, Dan Aykroyd, Garrett Morris, and Chevy Chase
As of September 2017, the late night live variety series Saturday Night Live (SNL) has featured 150 cast members. The ensemble was originally referred to as the "Not Ready For Prime Time Players."
Contents
1 All cast members
1.1 Timeline
2 Notable tenures
2.1 Longest tenures
2.2 Shortest tenures
2.3 Youngest cast members
2.4 Oldest cast members
2.5 President of the United States impressionists
3 Emmy Awards
4 Both cast and hosts
5 "SNL Curse"
6 See also
7 Notes
8 References
All cast members[edit]
The list below includes both repertory and featured players past and present, but omits SNL writers and others who were not listed as cast members during the show's credits. The dates given are those of the years they were part of the cast. The chart also shows whether the cast member has served as a guest host, appeared as the anchorperson of the "Weekend Update" segment (by any of its titles), or has been the subject of their own "Best of" home video collection. Many of the cast members were writers as well.
-
Performer
Years active
No. of seasons
Repertory player
Featured player only
"Weekend Update" anchor
Hosted
Best of...
Writer
Fred Armisen 2002–2013 11 Y Y
Dan Aykroyd 1975–1979 4 Y Y Y Y Y
Peter Aykroyd 1979–1980 1 Y Y
Morwenna Banks 1994–1995 1 Y
Vanessa Bayer 2010–2017 7 Y
Jim Belushi 1983–1985 2 Y Y
John Belushi 1975–1979 4 Y Y Y
Beck Bennett 2013–present 5 Y
Jim Breuer 1995–1998 3 Y
Paul Brittain 2010–2012 2 Y
A. Whitney Brown 1985–1991 6 Y Y
Aidy Bryant 2012–present 6 Y
Beth Cahill 1991–1992 1 Y
Dana Carvey 1986–1993 7 Y Y Y
Chevy Chase 1975-1977 2 Y Y Y Y Y
Michael Che 2014–present 4 Y Y Y
Ellen Cleghorne 1991–1995 4 Y
George Coe 1975–1976 1 Y
Billy Crystal 1984–1985 1 Y Y Y Y
Jane Curtin 1975–1980 5 Y Y
Joan Cusack 1985–1986 1 Y
Pete Davidson 2014–present 4 Y
Tom Davis 1977–1980 3 Y Y
Mikey Day 2016–present 2 Y Y
Denny Dillon 1980–1981 1 Y
Jim Downey 1979–1980 1 Y Y
Robert Downey Jr. 1985–1986 1 Y Y
Brian Doyle-Murray 1979–1980
1981–1982 2 Y Y Y
Rachel Dratch 1999–2006 7 Y
Robin Duke 1980–1984 4 Y Y
Nora Dunn 1985–1990 5 Y
Christine Ebersole 1981–1982 1 Y Y
Dean Edwards 2001–2003 2 Y
Abby Elliott 2008–2012 4 Y
Chris Elliott 1994–1995 1 Y
Jimmy Fallon 1998–2004 6 Y Y Y Y
Siobhan Fallon 1991–1992 1 Y
Chris Farley 1990–1995 5 Y Y Y
Will Ferrell 1995–2002 7 Y Y Y
Tina Fey 2000–2006 6 Y Y Y Y
Will Forte 2002–2010 8 Y
Al Franken 1977–1980
1985–1986
1988–1995 11 Y Y
Heidi Gardner 2017–present 1 Y
Janeane Garofalo 1994–1995 1 Y
Ana Gasteyer 1996–2002 6 Y
Gilbert Gottfried 1980–1981 1 Y
Mary Gross 1981–1985 4 Y Y Y
Christopher Guest 1984–1985 1 Y Y Y
Bill Hader 2005–2013 8 Y Y
Anthony Michael Hall 1985–1986 1 Y
Brad Hall 1982–1984 2 Y Y
Rich Hall 1984–1985 1 Y Y
Darrell Hammond 1995–2009 14 Y
Phil Hartman 1986–1994 8 Y Y Y Y
Jan Hooks 1986–1991 5 Y
Yvonne Hudson 1980–1981 1 Y
Melanie Hutsell 1991–1994 3 Y
Victoria Jackson 1986–1992 6 Y
Leslie Jones 2014–present 4 Y Y
Colin Jost 2013–present 5 Y Y Y
Chris Kattan 1995–2003 8 Y Y
Tim Kazurinsky 1980–1984 4 Y Y
Laura Kightlinger 1994–1995 1 Y Y
Taran Killam 2010–2016 6 Y
David Koechner 1995–1996 1 Y
Gary Kroeger 1982–1985 3 Y
Matthew Laurance 1980–1981 1 Y
Julia Louis-Dreyfus 1982–1985 3 Y Y
Jon Lovitz 1985–1990 5 Y Y Y
Norm Macdonald 1993–1998 5 Y Y Y Y
Gail Matthius 1980–1981 1 Y Y
Michael McKean 1993–1995 2 Y Y
Mark McKinney 1994–1997 3 Y
Kate McKinnon 2012–present 7 Y
Tim Meadows 1990–2000 10 Y Y Y
Laurie Metcalf 1980–1981 1 Y
Seth Meyers 2001–2014 13 Y Y Y
John Milhiser 2013–2014 1 Y
Dennis Miller 1985–1991 6 Y Y Y
Jerry Minor 2000–2001 1 Y Y
Finesse Mitchell 2003–2006 3 Y
Alex Moffat 2016–present 2 Y
Jay Mohr 1993–1995 2 Y Y
Kyle Mooney 2013–present 5 Y
Tracy Morgan 1996–2003 7 Y Y Y
Garrett Morris 1975–1980 5 Y Y
Bobby Moynihan 2008–2017 9 Y
Eddie Murphy 1980–1984 4 Y Y Y Y
Bill Murray 1976–1980 4 Y Y Y Y
Mike Myers 1988–1995 7 Y Y Y Y
Kevin Nealon 1986–1995 9 Y Y Y
Laraine Newman 1975–1980 5 Y
Don Novello 1979–1980
1985–1986 2 Y Y Y
Luke Null 2017–present 1 Y
Mike O'Brien 2013–2014 1 Y Y
Michael O'Donoghue 1975–1978 3 Y Y
Cheri Oteri 1995–2000 5 Y Y
Chris Parnell 1998–2006 8 Y
Nasim Pedrad 2009–2014 5 Y
Jay Pharoah 2010–2016 6 Y
Joe Piscopo 1980–1984 4 Y Y
Amy Poehler 2001–2009 8 Y Y Y Y
Emily Prager 1980–1981 1 Y
Randy Quaid 1985–1986 1 Y
Colin Quinn 1995–2000 5 Y Y Y
Gilda Radner 1975–1980 5 Y Y
Chris Redd 2017–present 1 Y
Jeff Richards 2001–2004 3 Y
Rob Riggle 2004–2005 1 Y
Ann Risley 1980–1981 1 Y
Tim Robinson 2012–2013 1 Y Y
Chris Rock 1990–1993 3 Y Y Y
Charles Rocket 1980–1981 1 Y Y
Tony Rosato 1980–1982 2 Y Y
Jon Rudnitsky 2015–2016 1 Y
Maya Rudolph 1999–2008 9 Y Y
Andy Samberg 2005–2012 7 Y Y Y
Adam Sandler 1990–1995 5 Y Y Y
Horatio Sanz 1998–2006 8 Y Y
Tom Schiller 1979–1980 1 Y Y
Rob Schneider 1990–1994 4 Y Y
Paul Shaffer 1979–1980 1 Y Y
Molly Shannon 1994–2001 7 Y Y Y
Harry Shearer 1979–1980
1984–1985 2 Y Y
Martin Short 1984–1985 1 Y Y Y
Sarah Silverman 1993–1994 1 Y Y Y
Jenny Slate 2009–2010 1 Y
Robert Smigel 1991–1993 2 Y Y
David Spade 1990–1996 6 Y Y Y Y
Pamela Stephenson 1984–1985 1 Y
Ben Stiller 1988–1989 1 Y Y
Cecily Strong 2012–present 6 Y Y
Jason Sudeikis 2004–2013 9 Y Y
Julia Sweeney 1990–1994 4 Y
Terry Sweeney 1985–1986 1 Y Y
Kenan Thompson 2003–present 15 Y
Danitra Vance 1985–1986 1 Y
Melissa Villaseñor 2016–present 2 Y
Dan Vitale 1985–1986 1 Y
Nancy Walls 1995–1996 1 Y
Michaela Watkins 2008–2009 1 Y
Damon Wayans 1985–1986 1 Y Y
Patrick Weathers 1980–1981 1 Y
Noël Wells 2013–2014 1 Y
Brooks Wheelan 2013–2014 1 Y
Kristen Wiig 2005–2012 7 Y Y
Casey Wilson 2007–2009 2 Y
Fred Wolf 1995–1997 2 Y Y
Sasheer Zamata 2014–2017 4 Y
Alan Zweibel 1979–1980 1 Y Y
Timeline[edit]
Lighter colors denote "featured players" versus repertory cast members.

Notable tenures[edit]
Longest tenures[edit]
These are the cast members who have spent at least ten seasons on the show.
Performer
No. of seasons
Notes
Kenan Thompson 15 Thompson holds the record of being the longest-tenured cast member in the show's history, having been a cast member since 2003. He is also the first person born after SNL's premiere in 1975 to have joined the cast (he was born in 1978). Thompson is also the only current cast member who was hired in the 2000s to still be on the show.
Darrell Hammond 14 Hired after a cast overhaul in 1995, he is the last cast member hired in the 1990s to leave the show, and the oldest cast member to leave the show (age 53 when he left the show in 2009). In 2014, Hammond returned to the show where he replaced Don Pardo as the show's announcer after Pardo's death, and often appears in sketches, reprising old roles such as Donald Trump and Bill Clinton.
Seth Meyers 13 He joined the show in 2001. In 2006, he starting anchoring Weekend Update and in 2012, his tenure on Weekend Update reached its seventh season, making him the longest-serving Weekend Update anchor (breaking the records held by Dennis Miller and Tina Fey). He continued to anchor Update until he left the show in February 2014 to take over hosting duties for Late Night.
Fred Armisen 11 Armisen joined the show in 2002, and left at the end of season 38 in 2013.
Al Franken Hired as a writer in the beginning of the series, as the show progressed, he and Tom Davis were allowed to perform material on-air sporadically, starting in 1977. He left the show in 1980, but returned to the show when Lorne Michaels came back in 1985, regaining his writing and on-air featured status, and came back in the finale episode of season 11 in 1986, and after a few years off, he came back for on-and-off featured status in 1988 and stayed until 1995. Later elected the junior United States Senator from Minnesota in 2009, and then he resigned in Jan. 2018.
Tim Meadows 10 Meadows joined the show in early 1991. He left the show at the end of the season 25, which ended in 2000, after ten seasons on the show.
Shortest tenures[edit]
These cast members spent less than a full 20-episode season on the show.[1]
Performer
No. of episodes
Notes
Emily Prager 0 Hired by Dick Ebersol to be a featured player, she appeared in a few sketches at dress rehearsal in what would be the final episode of season six, due to the Writers' Guild of America going on strike in 1981. She did not return to the SNL cast in season seven. This technically makes her the shortest tenured SNL cast member. Although she did not appear in the single episode for which she was credited as a featured player, she had appeared uncredited in five previous episodes.[2]
Laurie Metcalf 1 She also was hired as part of Ebersol's temporary season six cast following the termination of Jean Doumanian, and appeared on-camera in a Weekend Update piece. When the show was put on hiatus for retooling, she was not chosen to return to the show for the season seven cast.
Dan Vitale 3 Hired as an on-and-off featured player for season 11, he was only credited with appearing in three episodes throughout the season.
Morwenna Banks 4 She was hired as a repertory player for the last four episodes of season 20, but was let out of her contract as part of a major cast overhaul Lorne Michaels had planned for season 21.
Ben Stiller 4 Before becoming a cast member, he submitted a short film – a parody of the film The Color of Money – that was shown on the season 12 episode hosted by Charlton Heston. He was hired during season 14, but quit after four episodes due to creative differences. Despite this, he returned to host in 1998 and 2011.
Fred Wolf 4 He's been a writer since 1992. However, he became a featured player in near the end season 21 for the last four episodes, however, he only appeared and was credited for episodes 17, 18, and 20. His last episode was in the 3rd episode of the 22nd season. After that episode, he decided to leave the show for good.
Tom Schiller 7 One of the show writers who was upgraded to cast member status during season five, he left the show at the end of the season.
Patrick Weathers 7 Hired as a featured cast member for season six, he was fired along with many of Doumanian's cast.
George Coe 8 He was one of the original "Not-Ready-for-Primetime Players", because NBC wanted someone older in the cast. He was credited for only the first three episodes, though he continued to make several uncredited appearances throughout the first season. He was later known for voicing the valet Woodhouse in the animated series Archer.
Yvonne Hudson 8 She was a recurring extra during season five, and became the first black female cast member in season six. Like many of Doumanian's cast, she was fired mid-season.
Jim Downey 9 He was hired as one of many writers-turned-feature players in season five, and though he left the cast after the season, he returned to the show as a writer in the mid-1980s and has remained with it.
Matthew Laurance 10 Hired as a feature player during season six, he was fired as part of the mid-season overhaul.
Alan Zweibel 11 A writer for the show before joining the cast in season five, he left after the season finale.
Gilbert Gottfried 12 He joined the cast for season six and was fired as part of the mid-season overhaul.
Michael O'Donoghue 12 One of the original "Not Ready for Primetime Players" and the show's first head writer, he was dropped as a cast member after a few episodes. He remained with the show as a writer (leaving and returning twice) and occasional on-screen performer.
Ann Risley 12 She joined the cast for season six and was fired as part of the mid-season overhaul.
Charles Rocket 12 He joined the cast for season six and was fired as part of the mid-season overhaul, after having dropped an f-bomb one episode prior.
Damon Wayans 12 Hired for season 11 as a featured player, he was fired mid-season for improvising on the air. He returned as a guest to perform stand-up comedy on season 11's last episode and hosted SNL in 1995.
Beth Cahill 13 She joined the show during season 17 as an off-and-on featured player. She did not return the following season, as she was fired along with castmate Siobhan Fallon.
Denny Dillon 13 She joined the cast for season six and was let go after the finale as part of the cast overhaul. She auditioned for the show's first season, but did not make the cut.
Gail Matthius 13 She joined the cast for season six and was let go after the season ended.
Paul Shaffer 13 After being the band's pianist for the first five seasons, he joined the cast during season five, but left after the finale. He hosted SNL in 1987, making him the only member of the house band to do so.
Janeane Garofalo 14 She joined the cast during season 20, but quit mid-season due to creative differences.
Michaela Watkins 15 She joined the show on the first episode after the 2008 United States presidential election, then was let go before the start of season 35.
Peter Aykroyd 16 He joined the show midway through season five, but left at the end of the season, after only 16 episodes.
Youngest cast members[edit]
Performer
Age when joined show
Tenure
Anthony Michael Hall 17 years old 1985–1986
Eddie Murphy 19 years old 1980–1984
Robert Downey Jr. 20 years, 5 months 1985–1986
Pete Davidson 20 years, 10 months 2014–present
Abby Elliott 21 years, 5 months 2008–2012
Julia Louis-Dreyfus 21 years, 8 months 1982–1985
Sarah Silverman 22 years, 9 months 1993–1994
Jay Pharoah 22 years, 11 months 2010–2016
Oldest cast members[edit]
Performer
Age when joined show
Tenure
Leslie Jones 47 years old 2014–present
George Coe 46 years, 155 days 1975
Michael McKean 46 years, 147 days 1994–1995
Darrell Hammond 39 years old 1995–2009
Garrett Morris 38 years, 8 months 1975–1980
Phil Hartman 38 years, 1 month 1986–1994
Mike O'Brien 37 years old 2013–2014
Michaela Watkins 36 years, 11 months 2008–2009
Colin Quinn 36 years, 9 months 1996–2000
Christopher Guest 36 years, 8 months 1984–1985
Mikey Day 36 years, 7 months 2016-present
After 14 seasons, Hammond left as the show's oldest active cast member, ending his tenure at 53 years old during his final season in 2009.
President of the United States impressionists[edit]
Portraying the sitting President of the United States is considered "about as high [...] an honor that can be bestowed upon a cast member."[3]
President
Performer (years)
Gerald Ford Chevy Chase (1975–76)
Jimmy Carter Dan Aykroyd (1977–79)
Joe Piscopo (1980–81)
Ronald Reagan Charles Rocket (1981)
Joe Piscopo (1981–84)
Harry Shearer (1984)
Randy Quaid (1985–86)
Phil Hartman (1986–89)
George H. W. Bush Dana Carvey (1989–93)
President
Performer (years)
Bill Clinton Phil Hartman (1993–94)
Michael McKean (1994–95)
Darrell Hammond (1995–2001)
George W. Bush Will Ferrell (2001–2002)
Chris Parnell (2002–2003)
Darrell Hammond (2003)
Will Forte (2004–2006)
Jason Sudeikis (2006–2008)
Barack Obama Fred Armisen (2009–12)
Jay Pharoah (2012–16)
Donald Trump Alec Baldwin[n 1] (2017–present)
Darrell Hammond had the longest tenure portraying a U.S. president, with Bill Clinton from 1995–2001, and George W. Bush during 2003. Hammond also portrayed Richard Nixon in season 34, episode 12.
Michael McKean portrayed Bill Clinton during a brief period after Phil Hartman's departure. There was also a sketch featuring Chris Farley, David Spade, Chris Elliott, Adam Sandler, and Tim Meadows auditioning for the role of Clinton. There was also a gag in a 2001 sketch with Tracy Morgan filling in for Will Ferrell as George W. Bush.
Another noteworthy presidential portrayal was that of Dan Aykroyd as former president Richard Nixon from 1975–79.
Jim Carrey, while never having been an SNL cast member, portrayed Ronald Reagan in Funny or Die's Presidential Reunion of SNL Presidents (which reunited Chase as Ford, Aykroyd as Carter, Carvey as George H. W. Bush, Hammond as Clinton, Ferrell as George W. Bush, and Armisen as Obama), because two of the actors who previously portrayed Reagan had died since and the other three had declined to appear in the reunion. Carrey did, however, audition to be a cast member for the 1980–81 season; he hosted the show in May 1996, January 2011, and October 2014.
Donald Trump, having been a public figure before being president, was portrayed by several cast members over the years. He was portrayed by Phil Hartman (1988–90), Darrell Hammond (1999–11, 2015–16), Jason Sudeikis (2012) and Taran Killam (2015).
Emmy Awards[edit]
The Primetime Emmy Awards are presented by the American Academy of Television Arts & Sciences. These are the cast members who won or were nominated for an Emmy for their work while in the cast.
Year
Performer
Category
Result
Ref.
1976 Chevy Chase Performance in a Variety or Music Program - Supporting Actor Won
1977 Nominated
John Belushi Nominated
Gilda Radner Performance in a Variety or Music Program - Supporting Actress Nominated
1978 Dan Aykroyd Performance in a Variety or Music Program - Supporting Actror Nominated
John Belushi Nominated
Jane Curtin Performance in a Variety or Music Program - Supporting Actress Nominated
Gilda Radner Won
1984 Eddie Murphy Performance in a Variety or Music Program Nominated
Joe Piscopo Nominated
1985 Billy Crystal Nominated
1986 Jon Lovitz Nominated
1987 Nominated
1989 Dana Carvey Nominated
1990 Nominated
1991 Nominated
1992 Nominated
1993 Won
1994 Phil Hartman Nominated
Mike Myers Nominated
2000 Molly Shannon Nominated
2001 Will Ferrell Nominated
Year
Performer
Category
Result
Ref.
2008 Amy Poehler Supporting Actress in a Comedy Series Nominated
2009 Nominated
Kristen Wiig Nominated
2010 Nominated
2011 Nominated
2012 Nominated
Bill Hader Supporting Actor in a Comedy Series Nominated
2013 Nominated
2014 Kate McKinnon Supporting Actress in a Comedy Series Nominated
2015 Nominated
2016 Won
2017 Won [4]
Vanessa Bayer Nominated
Leslie Jones Nominated
Both cast and hosts[edit]
As of May 2016, there are 33 SNL hosts who, at one point in their careers, were either a repertory or featured member of the SNL cast.
Host
Number of
episodes
First hosted
Last hosted
Fred Armisen 1 May 21, 2016
Dan Aykroyd 1 May 17, 2003
Dana Carvey 4 October 22, 1994 February 5, 2011
Chevy Chase 8[5] February 18, 1978 February 15, 1997
Billy Crystal 2 March 17, 1984 May 12, 1984
Robert Downey Jr. 1 November 16, 1996
Jimmy Fallon 3 December 17, 2011 April 15, 2017
Chris Farley 1 October 25, 1997
Will Ferrell 4 May 14, 2005 January 27, 2018
Tina Fey 6 February 23, 2008 May 19, 2018
Bill Hader 2 October 11, 2014 March 17, 2018
Phil Hartman 2 March 23, 1996 November 23, 1996
Julia Louis-Dreyfus 3 May 13, 2006 April 16, 2016
Jon Lovitz 1 November 8, 1997
Norm Macdonald 1 October 23, 1999
Michael McKean 1 November 3, 1984
Tracy Morgan 2 March 14, 2009 October 17, 2015
Eddie Murphy 2 December 11, 1982 December 15, 1984
Bill Murray 5 March 7, 1981 February 20, 1999
Mike Myers 1 March 22, 1997
Don Novello 2 January 14, 1984 May 12, 1984
Amy Poehler 2 September 25, 2010 December 19, 2015
Chris Rock 2 November 2, 1996 November 1, 2014
Maya Rudolph 1 February 18, 2012
Andy Samberg 1 May 17, 2014
Paul Shaffer 1 January 31, 1987
Molly Shannon 1 May 12, 2007
Martin Short 3 December 6, 1986 December 15, 2012
Sarah Silverman 1 October 4, 2014
David Spade 2 November 7, 1998 March 12, 2005
Ben Stiller 2 October 24, 1998 October 8, 2011
Damon Wayans 1 April 8, 1995
Kristen Wiig 2 May 11, 2013 November 19, 2016
"SNL Curse"[edit]
Although SNL is best known as the launchpad for many successful careers, nine former cast members have died before the age of 60. This has given rise to a superstition known as the "Saturday Night Live Curse".[6][7][8]
Cast member
Age
Date of death
Cause of death
John Belushi 33 March 5, 1982 Belushi died of a drug overdose from a speedball injection (cocaine and heroin). His death led to the conviction of Cathy Smith for administering the fatal injection.
Gilda Radner 42 May 20, 1989 Radner died from ovarian cancer. She was originally scheduled to host the season 13 finale, a first for a former female cast member. However, SNL was canceled due to a Writer's Guild of America (WGA) strike. Radner's health worsened the following year. Moments before the season 14 finale, news broke of Radner's death. In lieu of the opening monologue Steve Martin, visibly shaken, introduced a replay of the "Dancing in the Dark" sketch he and Radner had performed in a 1978 episode;[9] her ex-husband G. E. Smith performed a musical tribute to Radner with the SNL band.
Danitra Vance 40 August 21, 1994 Vance died of breast cancer, which had returned after a remission three years earlier.
Michael O'Donoghue 54 November 8, 1994 O'Donoghue died from cerebral hemorrhage after suffering from severe chronic migraine headaches for most of his life. Bill Murray honored O'Donoghue's memory in an appearance on a season 20 episode[10] (hosted by Sarah Jessica Parker with musical guest R.E.M.) by replaying his sketch "Mr. Mike's Least Loved Bedtime Stories: The Soiled Kimono" from 1977.[11]
Chris Farley 33 December 18, 1997 Similar to Belushi, Farley died of a drug overdose from a speedball. His death occurred less than two months after he came back to host SNL, which turned out to be his final television appearance.
Phil Hartman 49 May 28, 1998 Hartman was murdered by his wife, Brynn, while he slept in his Encino, California home. Before committing this crime, Brynn had allegedly consumed a combination of cocaine, alcohol, and the antidepressant drug Zoloft, and later killed herself. During SNL's 25th anniversary special in 1999, several of Hartman's peers honored his memory by replaying his sketch "Love is a Dream" from 1988.
Charles Rocket 56 October 7, 2005 Rocket was found dead in his Canterbury, Connecticut backyard. Local police concluded his death a suicide; Rocket had allegedly taken his own life by slashing his throat with a box cutter.
Tom Davis 59 July 19, 2012 Davis died from head and neck cancer.
Jan Hooks 57 October 9, 2014 Hooks died of throat cancer after a long illness.[12]
See also[edit]
Wikimedia Commons has media related to Not Ready For Prime Time Players.
Saturday Night Live Band
List of Saturday Night Live guests
List of Saturday Night Live writers
Notes[edit]
Jump up ^ Alec Baldwin performed the impersonation on a recurring guest basis, and not as a member of the cast.
References[edit]
Jump up ^ Graham, Mark. "The Michaela Watkins Club: 21 Other SNL Cast Members Who Only Lasted a Season (or Less) – Vulture". Nymag.com. Retrieved 2011-05-16.
Jump up ^ Specifically, 21 May 1977 Archived October 2, 2013, at the Wayback Machine., 19 Nov 1977 Archived October 2, 2013, at the Wayback Machine., 10 Dec 1977 Archived October 2, 2013, at the Wayback Machine., 22 Apr 1978 Archived October 2, 2013, at the Wayback Machine., and 10 Oct 1981 Archived October 2, 2013, at the Wayback Machine..
Jump up ^ "SNL Presidents". Movieline.com. Retrieved 2011-05-16.
Jump up ^ Fair, Vanity. "Kate McKinnon's Emmy Speech Abruptly Cut Off as She Thanks Hillary Clinton". Vanity Fair.
Jump up ^ "Archived copy". Archived from the original on October 29, 2012. Retrieved August 15, 2013.
Jump up ^ "Is There A 'Saturday Night Live' Curse?". Archived from the original on October 20, 2013.
Jump up ^ Caroline Donnelly. "7 Tragic SNL Deaths".
Jump up ^ Robert Rorke. "9 'SNL' stars we lost too soon".
Jump up ^ "Saturday Night Live Transcripts, 77r: Steve Martin / The Blues Brothers, Dancing in the Dark".
Jump up ^ "Michael O'Donoghue Tribute". snltranscripts.jt.org.
Jump up ^ "SNL Transcripts: Miskel Spillman: 12/17/77: Least-Loved Bedtime Tale: The Soiled Kimono". snltranscripts.jt.org.
Jump up ^ Thomas, Mike (October 20, 2015). "The Laughs, Pathos, and Overwhelming Talent of Jan Hooks". Grantland. Retrieved January 8, 2016.
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Beck Bennett
Aidy Bryant
Michael Che
Pete Davidson
Leslie Jones
Colin Jost
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Kenan Thompson
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Heidi Gardner
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Throw-in
From Wikipedia, the free encyclopedia
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For boundary throw-in, see Laws of Australian Football.
This article needs additional citations for verification. Please help improve this article by adding citations to reliable sources. Unsourced material may be challenged and removed. (May 2009) (Learn how and when to remove this template message)
A player taking a correct throw-in during a game.
A throw-in is a method of restarting play in a game of association football (or soccer) when the ball has exited the side of the field of play.
Contents
[hide]
1 Procedure
2 Infringements
3 Historical origins of the throw-in
4 Unusual throw-ins
5 References
6 External links
Procedure[edit]
The throw-in is taken from the point where the ball crossed the touch-line, either on the ground or in the air, though typically a referee will tolerate small discrepancies between the position where the ball crossed the touch-line and the position of the throw-in. The throw-in is taken by the opponents of the player who last touched the ball when it crossed the touch-line.[1] Opposing players may stand at any distance from the thrower but no closer than 2 m (2.2 yd), so long as they are still on the pitch. A player may take a throw-in at a distance further back from the touch-line.
At the moment of delivering the ball, the thrower must face the field of play. He or she should have part of each foot either on the touch line or on the ground outside the touch line,[2] and use both hands to deliver the ball from behind and over the head.
The ball becomes in play as soon as it enters the field of play and leaves the hands of the thrower.
A goal cannot be scored directly from a throw-in; if a player throws the ball directly into their own goal without any other player touching it, the result is a corner kick to the opposing side.[3] Likewise an offensive goal cannot be scored directly from a throw in; the result in this case is a goal kick for the defending team.
A player may not be penalised for an offside offence when receiving the ball directly from a throw-in.[4] Skillful attackers can sometimes take advantage of this rule by getting behind the last defender(s) to receive the throw-in and having a clear path to goal.
The optimal release angle for attaining maximum distance is about 30 degrees above the horizontal, according to researchers at Brunel University.[5] According to the study, players are able to throw the ball with greater release velocity for lower angles. The optimal angle would be 45 degrees if the release velocity did not depend on the angle of throw, if the ball were thrown from ground level instead of above the head, and if there was not air drag.
Infringements[edit]
If an opposing player fails to respect the required distance (2 m) before the ball is in play or otherwise unfairly distracts or impedes the thrower, he or she may receive a caution (yellow card) for unsporting behavior.
If the thrower fails to deliver the ball per the required procedure, or delivers it from a point other than where the ball left the field of play, the throw-in is awarded to the opposing team. This is commonly known as a "foul throw",[6] though such throws are not considered fouls.
It is an infringement for the thrower to touch the ball a second time until it has been touched by another player; this is punishable by an indirect free kick to the opposing team from where the offence occurred, unless the second touch was also a more serious handling offence, in which case it is punishable by a direct free kick or penalty kick.
It is legal to throw the ball into the goal with no contact; however, a goal will not be scored directly from a throw in, nor can an own-goal, without being touched by a player. The restarts are a goal kick for the defending team and a corner kick for the attacking team, respectively. If any player (legally) touches the ball before it goes into the goal, then a goal is scored.
A goalkeeper cannot handle a ball thrown directly to him or her by a teammate. This cannot be circumvented by the keeper using the feet first before handling the ball. If this infringement occurs within the goalkeeper's penalty area, an indirect free kick is awarded. If the infringement occurs outside the goalkeeper's penalty area, a direct free kick is awarded.
Danielle Carter takes a throw-in for Arsenal Ladies
Historical origins of the throw-in[edit]
The modern throw-in comes from the nineteenth century English public school football games. In these codes of football a variety of methods of returning the ball into play from touch were used. The modern throw-in draws upon various aspects of a number of early English school games. For example, returning the ball by throwing it out was part of the Rugby and Cheltenham football rules. Like the modern throw-in, the direction was not specified. The Sheffield rules instigated the throw-in of the ball at right angles by the opposite side to the one that played it into touch.[7] The two-handed throw-in—called line-out—is part of rugby union football. That the first side reaching the ball must throw it out (at right angles, in this case) was part of the Football Association rules and the Rossall rules.
Unusual throw-ins[edit]
Rory Delap was highlighted for his throw-in technique: a former schoolboy javelin champion,[8] Delap was renowned for having one of the longest and most powerful throw-ins in football.[9]
A Notre Dame Fighting Irish women's soccer player attempting a flip throw
An uncommon but effective technique for delivering a faster than usual throw is the flip throw, popularized by Estonian player Risto Kallaste: in it the player, during the run-up, plants the ball on the ground, flips over it, and uses the momentum gained from the flip to increase the velocity of the ball.[10]
References[edit]
Jump up ^ FIFA, https://www.fifa.com/mm/document/affederation/federation/81/42/36/lotg_en.pdf, Laws of the Game, p.46, July 2008, accessed 13 May 2011
Jump up ^ Association, The Football. "The website for the English football association, the Emirates FA Cup and the England football team". www.thefa.com.
Jump up ^ FIFA.com. "Education & Technical - Referees - Laws of the Game - FIFA.com". FIFA.com.
Jump up ^ https://www.fifa.com/worldfootball/lawsofthegame/law/newsid=1290867.html
Jump up ^ Linthorne, Nicholas P.; Everett, David J. (19 January 2006). "Release angle for attaining maximum distance in the soccer throw-in". arXiv:physics/0601149  .
Jump up ^ "Soccer Rules Q&A Search AskTheref.com". asktheref.com.
Jump up ^ Football: The first hundred years. The untold story. Adrian Harvey. Routledge, Abingdon 2005 page 184
Jump up ^ Arsenal nemesis Rory Delap gives Stoke more than just long throwsThe Mirror. 3 November 2008. Retrieved 4 November 2008.
Jump up ^ Sunday World. p.115. 2 November 2008. Retrieved 2 November 2008.
Jump up ^ "The Art of the Flip Throw". 1 September 2011.
External links[edit]
FIFA Laws of the Game – Law 15)
Q&A on Throw Ins(from AskTheRef.com)
hide
v
t
e
Laws of the Game (rules of association football)
Terms
Law 1: The Field of Play
Law 2: The Ball
Law 3: The Number of Players
Law 4: The Players' Equipment
Law 5: The Referee
Law 6: The Other Match Officials
Law 7: The Duration of the Match
Law 8: The Start and Restart of Play
Law 9: The Ball In and Out of Play
Law 10: The Method of Scoring
Law 11: Offside
Law 12: Fouls and Misconduct
Law 13: Free kicks (direct and indirect)
Law 14: The Penalty Kick
Law 15: The Throw-In
Law 16: The Goal Kick
Law 17: The Corner Kick
Comparisons
Football and rugby union
Football and futsal
IFAB
The Football Association
Scottish Football Association
Football Association of Wales
Irish Football Association
FIFA
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text:
Igneous rock
From Wikipedia, the free encyclopedia
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Geologic provinces of the World (USGS)
Shield
Platform
Orogen
Basin
Large igneous province
Extended crust
Oceanic crust:
0–20 Ma
20–65 Ma
>65 Ma
Igneous rock (derived from the Latin word ignis meaning fire), or magmatic rock, is one of the three main rock types, the others being sedimentary and metamorphic. Igneous rock is formed through the cooling and solidification of magma or lava. The magma can be derived from partial melts of existing rocks in either a planet's mantle or crust. Typically, the melting is caused by one or more of three processes: an increase in temperature, a decrease in pressure, or a change in composition. Solidification into rock occurs either below the surface as intrusive rocks or on the surface as extrusive rocks. Igneous rock may form with crystallization to form granular, crystalline rocks, or without crystallization to form natural glasses.
Contents
[hide]
1 Geological significance
2 Geological setting
2.1 Intrusive
2.2 Extrusive
3 Classification
3.1 Texture
3.2 Chemical classification and petrology
3.3 History of classification
4 Mineralogical classification
4.1 Example of classification
5 Magma origination
5.1 Decompression
5.2 Effects of water and carbon dioxide
5.3 Temperature increase
5.4 Magma evolution
6 Etymology
7 See also
8 Notes
9 References
10 Additional Reading
11 External links
Geological significance
Igneous and metamorphic rocks make up 90–95% of the top 16 km of the Earth's crust by volume.[1] Igneous rocks form about 15% of the Earth's current land surface.[note 1] Most of the Earth's oceanic crust is made of igneous rock.
Igneous rocks are also geologically important because:
their minerals and global chemistry give information about the composition of the mantle, from which some igneous rocks are extracted, and the temperature and pressure conditions that allowed this extraction, and/or of other pre-existing rock that melted;
their absolute ages can be obtained from various forms of radiometric dating and thus can be compared to adjacent geological strata, allowing a time sequence of events;
their features are usually characteristic of a specific tectonic environment, allowing tectonic reconstitutions (see plate tectonics);
in some special circumstances they host important mineral deposits (ores): for example, tungsten, tin, and uranium are commonly associated with granites and diorites, whereas ores of chromium and platinum are commonly associated with gabbros.
Geological setting
Forming of igneous rock
In terms of modes of occurrence, igneous rocks can be either intrusive (plutonic and hypabyssal) or extrusive (volcanic).
Intrusive
Close-up of granite (an intrusive igneous rock) exposed in Chennai, India.
Intrusive igneous rocks are formed from magma that cools and solidifies within the crust of a planet, surrounded by pre-existing rock (called country rock); the magma cools slowly and, as a result, these rocks are coarse-grained. The mineral grains in such rocks can generally be identified with the naked eye. Intrusive rocks can also be classified according to the shape and size of the intrusive body and its relation to the other formations into which it intrudes. Typical intrusive formations are batholiths, stocks, laccoliths, sills and dikes. When the magma solidifies within the earth's crust, it cools slowly forming coarse textured rocks, such as granite, gabbro, or diorite.
The central cores of major mountain ranges consist of intrusive igneous rocks, usually granite. When exposed by erosion, these cores (called batholiths) may occupy huge areas of the Earth's surface.
Intrusive igneous rocks that form at depth within the crust are termed plutonic (or abyssal) rocks and are usually coarse-grained. Intrusive igneous rocks that form near the surface are termed subvolcanic or hypabyssal rocks and they are usually medium-grained. Hypabyssal rocks are less common than plutonic or volcanic rocks and often form dikes, sills, laccoliths, lopoliths, or phacoliths.
Extrusive
Extrusive igneous rock is made from lava released by volcanoes
Sample of basalt (an extrusive igneous rock), found in Massachusetts
Extrusive igneous rocks, also known as volcanic rocks, are formed at the crust's surface as a result of the partial melting of rocks within the mantle and crust. Extrusive igneous rocks cool and solidify quicker than intrusive igneous rocks. They are formed by the cooling of molten magma on the earth's surface. The magma, which is brought to the surface through fissures or volcanic eruptions, solidifies at a faster rate. Hence such rocks are smooth, crystalline and fine-grained. Basalt is a common extrusive igneous rock and forms lava flows, lava sheets and lava plateaus. Some kinds of basalt solidify to form long polygonal columns. The Giant's Causeway in Antrim, Northern Ireland is an example.
The molten rock, with or without suspended crystals and gas bubbles, is called magma. It rises because it is less dense than the rock from which it was created. When magma reaches the surface from beneath water or air, it is called lava. Eruptions of volcanoes into air are termed subaerial, whereas those occurring underneath the ocean are termed submarine. Black smokers and mid-ocean ridge basalt are examples of submarine volcanic activity.
The volume of extrusive rock erupted annually by volcanoes varies with plate tectonic setting. Extrusive rock is produced in the following proportions:[3]
divergent boundary: 73%
convergent boundary (subduction zone): 15%
hotspot: 12%.
Magma that erupts from a volcano behaves according to its viscosity, determined by temperature, composition, crystal content and the amount of silica. High-temperature magma, most of which is basaltic in composition, behaves in a manner similar to thick oil and, as it cools, treacle. Long, thin basalt flows with pahoehoe surfaces are common. Intermediate composition magma, such as andesite, tends to form cinder cones of intermingled ash, tuff and lava, and may have a viscosity similar to thick, cold molasses or even rubber when erupted. Felsic magma, such as rhyolite, is usually erupted at low temperature and is up to 10,000 times as viscous as basalt. Volcanoes with rhyolitic magma commonly erupt explosively, and rhyolitic lava flows are typically of limited extent and have steep margins, because the magma is so viscous.
Felsic and intermediate magmas that erupt often do so violently, with explosions driven by the release of dissolved gases—typically water vapour, but also carbon dioxide. Explosively erupted pyroclastic material is called tephra and includes tuff, agglomerate and ignimbrite. Fine volcanic ash is also erupted and forms ash tuff deposits, which can often cover vast areas.
Because lava usually cools and crystallizes rapidly, it is usually fine-grained. If the cooling has been so rapid as to prevent the formation of even small crystals after extrusion, the resulting rock may be mostly glass (such as the rock obsidian). If the cooling of the lava happened more slowly, the rock would be coarse-grained.
Because the minerals are mostly fine-grained, it is much more difficult to distinguish between the different types of extrusive igneous rocks than between different types of intrusive igneous rocks. Generally, the mineral constituents of fine-grained extrusive igneous rocks can only be determined by examination of thin sections of the rock under a microscope, so only an approximate classification can usually be made in the field.
Classification
Igneous rocks are classified according to mode of occurrence, texture, mineralogy, chemical composition, and the geometry of the igneous body.
The classification of the many types of different igneous rocks can provide us with important information about the conditions under which they formed. Two important variables used for the classification of igneous rocks are particle size, which largely depends on the cooling history, and the mineral composition of the rock. Feldspars, quartz or feldspathoids, olivines, pyroxenes, amphiboles, and micas are all important minerals in the formation of almost all igneous rocks, and they are basic to the classification of these rocks. All other minerals present are regarded as nonessential in almost all igneous rocks and are called accessory minerals. Types of igneous rocks with other essential minerals are very rare, and these rare rocks include those with essential carbonates.
In a simplified classification, igneous rock types are separated on the basis of the type of feldspar present, the presence or absence of quartz, and in rocks with no feldspar or quartz, the type of iron or magnesium minerals present. Rocks containing quartz (silica in composition) are silica-oversaturated. Rocks with feldspathoids are silica-undersaturated, because feldspathoids cannot coexist in a stable association with quartz.
Igneous rocks that have crystals large enough to be seen by the naked eye are called phaneritic; those with crystals too small to be seen are called aphanitic. Generally speaking, phaneritic implies an intrusive origin; aphanitic an extrusive one.
An igneous rock with larger, clearly discernible crystals embedded in a finer-grained matrix is termed porphyry. Porphyritic texture develops when some of the crystals grow to considerable size before the main mass of the magma crystallizes as finer-grained, uniform material.
Igneous rocks are classified on the basis of texture and composition. Texture refers to the size, shape, and arrangement of the mineral grains or crystals of which the rock is composed.
Texture
Gabbro specimen showing phaneritic texture; Rock Creek Canyon, eastern Sierra Nevada, California; scale bar is 2.0 cm.
Main article: Rock microstructure
Texture is an important criterion for the naming of volcanic rocks. The texture of volcanic rocks, including the size, shape, orientation, and distribution of mineral grains and the intergrain relationships, will determine whether the rock is termed a tuff, a pyroclastic lava or a simple lava.
However, the texture is only a subordinate part of classifying volcanic rocks, as most often there needs to be chemical information gleaned from rocks with extremely fine-grained groundmass or from airfall tuffs, which may be formed from volcanic ash.
Textural criteria are less critical in classifying intrusive rocks where the majority of minerals will be visible to the naked eye or at least using a hand lens, magnifying glass or microscope. Plutonic rocks also tend to be less texturally varied and less prone to gaining structural fabrics. Textural terms can be used to differentiate different intrusive phases of large plutons, for instance porphyritic margins to large intrusive bodies, porphyry stocks and subvolcanic dikes (apophyses). Mineralogical classification is most often used to classify plutonic rocks. Chemical classifications are preferred to classify volcanic rocks, with phenocryst species used as a prefix, e.g. "olivine-bearing picrite" or "orthoclase-phyric rhyolite".
see also List of rock textures and Igneous textures
Basic classification scheme for igneous rocks on their mineralogy. If the approximate volume fractions of minerals in the rock are known, the rock name and silica content can be read off the diagram. This is not an exact method, because the classification of igneous rocks also depends on other components than silica, yet in most cases it is a good first guess.
Chemical classification and petrology
Total alkali versus silica classification scheme (TAS) as proposed in Le Maitre's 2002 Igneous Rocks - A classification and glossary of terms[4]:237
Igneous rocks can be classified according to chemical or mineralogical parameters.
Chemical: total alkali-silica content (TAS diagram) for volcanic rock classification used when modal or mineralogic data is unavailable:
felsic igneous rocks containing a high silica content, greater than 63% SiO2 (examples granite and rhyolite),
intermediate igneous rocks containing between 52–63% SiO2 (example andesite and dacite),
mafic igneous rocks have low silica 45–52% and typically high iron – magnesium content (example gabbro and basalt),
ultramafic rock igneous rocks with less than 45% silica (examples picrite, komatiite and peridotite),
alkalic igneous rocks with 5–15% alkali (K2O + Na2O) content or with a molar ratio of alkali to silica greater than 1:6 (examples phonolite and trachyte).
Chemical classification also extends to differentiating rocks that are chemically similar according to the TAS diagram, for instance:
Ultrapotassic – rocks containing molar K2O/Na2O >3.
Peralkaline – rocks containing molar (K2O + Na2O)/Al2O3 >1.
Peraluminous – rocks containing molar (K2O + Na2O)/Al2O3 <1.
An idealized mineralogy (the normative mineralogy) can be calculated from the chemical composition, and the calculation is useful for rocks too fine-grained or too altered for identification of minerals that crystallized from the melt. For instance, normative quartz classifies a rock as silica-oversaturated; an example is rhyolite. In an older terminology, silica oversaturated rocks were called silicic or acidic where the SiO2 was greater than 66% and the family term quartzolite was applied to the most silicic. A normative feldspathoid classifies a rock as silica-undersaturated; an example is nephelinite.
History of classification
In 1902, a group of American petrographers proposed that all existing classifications of igneous rocks should be discarded and replaced by a "quantitative" classification based on chemical analysis. They showed how vague, and often unscientific, much of the existing terminology was and argued that as the chemical composition of an igneous rock was its most fundamental characteristic, it should be elevated to prime position.
Geological occurrence, structure, mineralogical constitution—the hitherto accepted criteria for the discrimination of rock species—were relegated to the background. The completed rock analysis is first to be interpreted in terms of the rock-forming minerals which might be expected to be formed when the magma crystallizes, e.g., quartz feldspars, olivine, akermannite, Feldspathoids, magnetite, corundum, and so on, and the rocks are divided into groups strictly according to the relative proportion of these minerals to one another.[5][6]
Mineralogical classification
For volcanic rocks, mineralogy is important in classifying and naming lavas. The most important criterion is the phenocryst species, followed by the groundmass mineralogy. Often, where the groundmass is aphanitic, chemical classification must be used to properly identify a volcanic rock.
Mineralogic contents – felsic versus mafic
felsic rock, highest content of silicon, with predominance of quartz, alkali feldspar and/or feldspathoids: the felsic minerals; these rocks (e.g., granite, rhyolite) are usually light coloured, and have low density.
mafic rock, lesser content of silicon relative to felsic rocks, with predominance of mafic minerals pyroxenes, olivines and calcic plagioclase; these rocks (example, basalt, gabbro) are usually dark coloured, and have a higher density than felsic rocks.
ultramafic rock, lowest content of silicon, with more than 90% of mafic minerals (e.g., dunite).
For intrusive, plutonic and usually phaneritic igneous rocks (where all minerals are visible at least via microscope), the mineralogy is used to classify the rock. This usually occurs on ternary diagrams, where the relative proportions of three minerals are used to classify the rock.
The following table is a simple subdivision of igneous rocks according to both their composition and mode of occurrence.
Composition
Mode of occurrence
Felsic Intermediate Mafic Ultramafic
Intrusive Granite Diorite Gabbro Peridotite
Extrusive Rhyolite Andesite Basalt Komatiite
For a more detailed classification see QAPF diagram.
Example of classification
Granite is an igneous intrusive rock (crystallized at depth), with felsic composition (rich in silica and predominately quartz plus potassium-rich feldspar plus sodium-rich plagioclase) and phaneritic, subeuhedral texture (minerals are visible to the unaided eye and commonly some of them retain original crystallographic shapes).
Magma origination
The Earth's crust averages about 35 kilometers thick under the continents, but averages only some 7–10 kilometers beneath the oceans. The continental crust is composed primarily of sedimentary rocks resting on a crystalline basement formed of a great variety of metamorphic and igneous rocks, including granulite and granite. Oceanic crust is composed primarily of basalt and gabbro. Both continental and oceanic crust rest on peridotite of the mantle.
Rocks may melt in response to a decrease in pressure, to a change in composition (such as an addition of water), to an increase in temperature, or to a combination of these processes.
Other mechanisms, such as melting from a meteorite impact, are less important today, but impacts during the accretion of the Earth led to extensive melting, and the outer several hundred kilometers of our early Earth was probably an ocean of magma. Impacts of large meteorites in the last few hundred million years have been proposed as one mechanism responsible for the extensive basalt magmatism of several large igneous provinces.
Decompression
Decompression melting occurs because of a decrease in pressure.[7]
The solidus temperatures of most rocks (the temperatures below which they are completely solid) increase with increasing pressure in the absence of water. Peridotite at depth in the Earth's mantle may be hotter than its solidus temperature at some shallower level. If such rock rises during the convection of solid mantle, it will cool slightly as it expands in an adiabatic process, but the cooling is only about 0.3 °C per kilometer. Experimental studies of appropriate peridotite samples document that the solidus temperatures increase by 3 °C to 4 °C per kilometer. If the rock rises far enough, it will begin to melt. Melt droplets can coalesce into larger volumes and be intruded upwards. This process of melting from the upward movement of solid mantle is critical in the evolution of the Earth.
Decompression melting creates the ocean crust at mid-ocean ridges. It also causes volcanism in intraplate regions, such as Europe, Africa and the Pacific sea floor. There, it is variously attributed either to the rise of mantle plumes (the "Plume hypothesis") or to intraplate extension (the "Plate hypothesis").[8]
Effects of water and carbon dioxide
The change of rock composition most responsible for the creation of magma is the addition of water. Water lowers the solidus temperature of rocks at a given pressure. For example, at a depth of about 100 kilometers, peridotite begins to melt near 800 °C in the presence of excess water, but near or above about 1,500 °C in the absence of water.[9] Water is driven out of the oceanic lithosphere in subduction zones, and it causes melting in the overlying mantle. Hydrous magmas composed of basalt and andesite are produced directly and indirectly as results of dehydration during the subduction process. Such magmas, and those derived from them, build up island arcs such as those in the Pacific Ring of Fire. These magmas form rocks of the calc-alkaline series, an important part of the continental crust.
The addition of carbon dioxide is relatively a much less important cause of magma formation than the addition of water, but genesis of some silica-undersaturated magmas has been attributed to the dominance of carbon dioxide over water in their mantle source regions. In the presence of carbon dioxide, experiments document that the peridotite solidus temperature decreases by about 200 °C in a narrow pressure interval at pressures corresponding to a depth of about 70 km. At greater depths, carbon dioxide can have more effect: at depths to about 200 km, the temperatures of initial melting of a carbonated peridotite composition were determined to be 450 °C to 600 °C lower than for the same composition with no carbon dioxide.[10] Magmas of rock types such as nephelinite, carbonatite, and kimberlite are among those that may be generated following an influx of carbon dioxide into mantle at depths greater than about 70 km.
Temperature increase
Increase in temperature is the most typical mechanism for formation of magma within continental crust. Such temperature increases can occur because of the upward intrusion of magma from the mantle. Temperatures can also exceed the solidus of a crustal rock in continental crust thickened by compression at a plate boundary. The plate boundary between the Indian and Asian continental masses provides a well-studied example, as the Tibetan Plateau just north of the boundary has crust about 80 kilometers thick, roughly twice the thickness of normal continental crust. Studies of electrical resistivity deduced from magnetotelluric data have detected a layer that appears to contain silicate melt and that stretches for at least 1,000 kilometers within the middle crust along the southern margin of the Tibetan Plateau.[11] Granite and rhyolite are types of igneous rock commonly interpreted as products of the melting of continental crust because of increases in temperature. Temperature increases also may contribute to the melting of lithosphere dragged down in a subduction zone.
Magma evolution
Schematic diagrams showing the principles behind fractional crystallisation in a magma. While cooling, the magma evolves in composition because different minerals crystallize from the melt. 1: olivine crystallizes; 2: olivine and pyroxene crystallize; 3: pyroxene and plagioclase crystallize; 4: plagioclase crystallizes. At the bottom of the magma reservoir, a cumulate rock forms.
Main article: Igneous differentiation
Most magmas only entirely melt for small parts of their histories. More typically, they are mixes of melt and crystals, and sometimes also of gas bubbles. Melt, crystals, and bubbles usually have different densities, and so they can separate as magmas evolve.
As magma cools, minerals typically crystallize from the melt at different temperatures (fractional crystallization). As minerals crystallize, the composition of the residual melt typically changes. If crystals separate from the melt, then the residual melt will differ in composition from the parent magma. For instance, a magma of gabbroic composition can produce a residual melt of granitic composition if early formed crystals are separated from the magma. Gabbro may have a liquidus temperature near 1,200 °C, and the derivative granite-composition melt may have a liquidus temperature as low as about 700 °C. Incompatible elements are concentrated in the last residues of magma during fractional crystallization and in the first melts produced during partial melting: either process can form the magma that crystallizes to pegmatite, a rock type commonly enriched in incompatible elements. Bowen's reaction series is important for understanding the idealised sequence of fractional crystallisation of a magma.
Magma composition can be determined by processes other than partial melting and fractional crystallization. For instance, magmas commonly interact with rocks they intrude, both by melting those rocks and by reacting with them. Magmas of different compositions can mix with one another. In rare cases, melts can separate into two immiscible melts of contrasting compositions.
There are relatively few minerals that are important in the formation of common igneous rocks, because the magma from which the minerals crystallize is rich in only certain elements: silicon, oxygen, aluminium, sodium, potassium, calcium, iron, and magnesium. These are the elements that combine to form the silicate minerals, which account for over ninety percent of all igneous rocks. The chemistry of igneous rocks is expressed differently for major and minor elements and for trace elements. Contents of major and minor elements are conventionally expressed as weight percent oxides (e.g., 51% SiO2, and 1.50% TiO2). Abundances of trace elements are conventionally expressed as parts per million by weight (e.g., 420 ppm Ni, and 5.1 ppm Sm). The term "trace element" is typically used for elements present in most rocks at abundances less than 100 ppm or so, but some trace elements may be present in some rocks at abundances exceeding 1,000 ppm. The diversity of rock compositions has been defined by a huge mass of analytical data—over 230,000 rock analyses can be accessed on the web through a site sponsored by the U. S. National Science Foundation (see the External Link to EarthChem).
Etymology
The word "igneous" is derived from the Latin ignis, meaning "of fire". Volcanic rocks are named after Vulcan, the Roman name for the god of fire. Intrusive rocks are also called "plutonic" rocks, named after Pluto, the Roman god of the underworld.
See also
Large igneous province
List of rock types
Metamorphic rock
Migmatite
Petrology
Sedimentary rock
Notes
Jump up ^ 15% is the arithmetic sum of the area for intrusive plutonic rock (7%) plus the area for extrusive volcanic rock (8%).[2]
References
Jump up ^ Prothero, Donald R.; Schwab, Fred (2004). Sedimentary geology : an introduction to sedimentary rocks and stratigraphy (2nd ed.). New York: Freeman. p. 12. ISBN 978-0-7167-3905-0.
Jump up ^ Wilkinson, Bruce H.; McElroy, Brandon J.; Kesler, Stephen E.; Peters, Shanan E.; Rothman, Edward D. (2008). "Global geologic maps are tectonic speedometers—Rates of rock cycling from area-age frequencies". Geological Society of America Bulletin. 121 (5–6): 760–779. doi:10.1130/B26457.1.
Jump up ^ Fisher, R. V. & Schmincke H.-U., (1984) Pyroclastic Rocks, Berlin, Springer-Verlag
Jump up ^ Ridley, W. I., 2012, Petrology of Igneous Rocks, Volcanogenic Massive Sulfide Occurrence Model, USGS Scientific Report 2010-5070-C, Chapter 15.
Jump up ^ Cross, W. et al. (1903) Quantitative Classification of Igneous Rocks, Chicago, University of Chicago Press
Jump up ^ One or more of the preceding sentences incorporates text from a publication now in the public domain: Chisholm, Hugh, ed. (1911). "Petrology". Encyclopædia Britannica. 21 (11th ed.). Cambridge University Press. pp. 323–333.
Jump up ^ Geoff C. Brown; C. J. Hawkesworth; R. C. L. Wilson (1992). Understanding the Earth (2nd ed.). Cambridge University Press. p. 93. ISBN 0-521-42740-1.
Jump up ^ Foulger, G.R. (2010). Plates vs. Plumes: A Geological Controversy. Wiley-Blackwell. ISBN 978-1-4051-6148-0.
Jump up ^ T. L. Grove, N. Chatterjee, S. W. Parman, and E. Medard, (2006)The influence of H2O on mantle wedge melting. Earth and Planetary Science Letters, v. 249, p. 74-89
Jump up ^ R. Dasgupta and M. M. Hirschmann (2007) Effect of variable carbonate concentration on the solidus of mantle peridotite. American Mineralogist, v. 92, p. 370-379
Jump up ^ M. J. Unsworth et al. (2005) Crustal rheology of the Himalaya and Southern Tibet inferred from magnetotelluric data. Nature, v. 438, p. 78-81
Additional Reading
R. W. Le Maitre (editor) (2002) Igneous Rocks: A Classification and Glossary of Terms, Recommendations of the International Union of Geological Sciences, Subcommission of the Systematics of Igneous Rocks., Cambridge, Cambridge University Press ISBN 0-521-66215-X
External links
The Wikibook Historical Geology has a page on the topic of: Igneous rocks and stratigraphy
The Wikibook Historical Geology has a page on the topic of: Igneous rocks
USGS Igneous Rocks
Igneous rock classification flowchart
Igneous Rocks Tour, an introduction to Igneous Rocks
The IUGS systematics of igneous rocks
Wikimedia Commons has media related to Igneous rocks.
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Common igneous rocks classified by silicon dioxide content
Type Ultramafic
<45% SiO2 Mafic
45–52% SiO2 Intermediate
52–63% SiO2 Intermediate–felsic
63–69% SiO2 Felsic
>69% SiO2
Volcanic rocks:
Subvolcanic rocks:
Plutonic rocks:
Komatiite, Picrite basalt
Kimberlite, Lamproite
Peridotite
Basalt
Diabase (Dolerite)
Gabbro
Andesite
Microdiorite
Diorite
Dacite
Microgranodiorite
Granodiorite
Rhyolite
Microgranite, Aplite
Granite
Authority control
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NDL: 00565095
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/wiki/Wikipedia:File_Upload_Wizard
Upload files [ctrl-alt-u]
u

values: A list of all special pages [ctrl-alt-q]

values: Permanent link to this revision of the page

values: Link to connected data repository item [ctrl-alt-g]

values: Printable version of this page [ctrl-alt-p]

values: portal navigation p-wikibase-otherprojects p-wikibase-otherprojects-label

values:
interlanguage-link interwiki-af
display: none;

values: صخر ناري – Arabic

values:
interlanguage-link interwiki-an
display: none;

values:
interlanguage-link interwiki-ast
display: none;

values: আগ্নেয় শিলা – Bangla

values:
interlanguage-link interwiki-bn
display: none;

values:
interlanguage-link interwiki-zh-min-nan
display: none;

values: Магмалы тау тоҡомдары – Bashkir

values:
interlanguage-link interwiki-ba
display: none;

values: Магматычныя горныя пароды – Belarusian

values:
interlanguage-link interwiki-be
display: none;

values: Магматычныя горныя пароды – Belarusian (Taraškievica orthography)

values:
interlanguage-link interwiki-be-x-old
display: none;

values: Магмени скали – Bulgarian

values:
interlanguage-link interwiki-bg
display: none;

values:
interlanguage-link interwiki-bs
display: none;

values:
interlanguage-link interwiki-ca
display: none;

values:
interlanguage-link interwiki-cs
display: none;

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interlanguage-link interwiki-cy
display: none;

values:
interlanguage-link interwiki-da
display: none;

values:
interlanguage-link interwiki-de
display: none;

values:
https://et.wikipedia.org/wiki/Tardkivim
Tardkivim – Estonian
et
et
interlanguage-link-target

values:
interlanguage-link interwiki-et
display: none;

values: Εκρηξιγενές πέτρωμα – Greek

values:
interlanguage-link interwiki-el
display: none;

values:
interlanguage-link interwiki-eo
display: none;

values:
interlanguage-link interwiki-eu
display: none;

values: سنگ آذرین – Persian

values:
interlanguage-link interwiki-fa
display: none;

values:
interlanguage-link interwiki-fr
display: none;

values:
interlanguage-link interwiki-ga
display: none;

values:
interlanguage-link interwiki-gd
display: none;

values:
interlanguage-link interwiki-gl
display: none;

values:
interlanguage-link interwiki-ko
display: none;

values: Մագմատիկ ապարներ – Armenian

values:
interlanguage-link interwiki-hy
display: none;

values: आग्नेय शैल – Hindi

values:
interlanguage-link interwiki-hr
display: none;

values:
interlanguage-link interwiki-is
display: none;

values:
interlanguage-link interwiki-it
display: none;

values: סלע יסוד – Hebrew

values:
interlanguage-link interwiki-he
display: none;

values:
https://jv.wikipedia.org/wiki/Watu_beku
Watu beku – Javanese
jv
jv
interlanguage-link-target

values:
interlanguage-link interwiki-jv
display: none;

values: ಅಗ್ನಿಶಿಲೆ – Kannada

values:
interlanguage-link interwiki-kn
display: none;

values: მაგმური ქანები – Georgian

values:
interlanguage-link interwiki-ka
display: none;

values: Магмалық тау жыныстары – Kazakh

values:
interlanguage-link interwiki-kk
display: none;

values:
interlanguage-link interwiki-ht
display: none;

values: Магма кендери – Kyrgyz

values:
interlanguage-link interwiki-ky
display: none;

values:
interlanguage-link interwiki-la
display: none;

values:
interlanguage-link interwiki-lv
display: none;

values:
interlanguage-link interwiki-lt
display: none;

values:
interlanguage-link interwiki-jbo
display: none;

values:
interlanguage-link interwiki-hu
display: none;

values: Магматска карпа – Macedonian

values:
interlanguage-link interwiki-mk
display: none;

values: ആഗ്നേയശില – Malayalam

values:
interlanguage-link interwiki-ml
display: none;

values: Магмын чулуулаг – Mongolian

values:
interlanguage-link interwiki-mn
display: none;

values: မီးသင့်ကျောက် – Burmese

values:
interlanguage-link interwiki-my
display: none;

values: आग्नेय चट्टान – Nepali

values:
interlanguage-link interwiki-ne
display: none;

values:
interlanguage-link interwiki-ja
display: none;

values:
interlanguage-link interwiki-nn
display: none;

values:
interlanguage-link interwiki-oc
display: none;

values:
interlanguage-link interwiki-uz
display: none;

values: ਆਤਸ਼ੀ ਚਟਾਨ – Punjabi

values:
interlanguage-link interwiki-pa
display: none;

values:
interlanguage-link interwiki-pnb
display: none;

values:
https://nds.wikipedia.org/wiki/Magmatit
Magmatit – Low German
nds
nds
interlanguage-link-target

values:
interlanguage-link interwiki-nds
display: none;

values:
interlanguage-link interwiki-pl
display: none;

values:
interlanguage-link interwiki-pt
display: none;

values: Магматические горные породы – Russian

values:
interlanguage-link interwiki-sco
display: none;

values:
interlanguage-link interwiki-sk
display: none;

values: interlanguage-link interwiki-sl badge-Q17437796 badge-featuredarticle

values: Магматске стене – Serbian

values:
interlanguage-link interwiki-sh
display: none;

values:
interlanguage-link interwiki-su
display: none;

values:
https://fi.wikipedia.org/wiki/Magmakivi
Magmakivi – Finnish
fi
fi
interlanguage-link-target

values:
interlanguage-link interwiki-fi
display: none;

values: தீப்பாறை – Tamil

values:
interlanguage-link interwiki-ta
display: none;

values: หินอัคนี – Thai

values:
interlanguage-link interwiki-th
display: none;

values: Ҷинсҳои кӯҳии магматикӣ – Tajik

values:
interlanguage-link interwiki-tg
display: none;

values: Магматичні гірські породи – Ukrainian

values: آتشی چٹان – Urdu

values: mediawiki ltr sitedir-ltr mw-hide-empty-elt ns-0 ns-subject page-Igneous_rock rootpage-Igneous_rock skin-vector action-view