document_title: Hawaii hotspot

question_text: the state of hawai'i is located on which tectonic plate

text: Hawaii hotspot

text: Theories[edit]

text: Tectonic plates generally focus deformation and volcanism at plate boundaries. However, the Hawaii hotspot is more than 3,200 kilometers (1,988 mi) from the nearest plate boundary;[1] while studying it in 1963, Canadian geophysicist J. Tuzo Wilson proposed the hotspot theory to explain these zones of volcanism so far from regular conditions,[3] a theory that has since come into wide acceptance.[4]

text: Wilson's stationary hotspot theory[edit]

text: Wilson proposed that mantle convection produces small, hot buoyant upwellings under the Earth's surface; these thermally active mantle plumes supply magma which in turn sustains long-lasting volcanic activity. This "mid-plate" volcanism builds peaks that rise from relatively featureless sea floor, initially as seamounts and later as fully-fledged volcanic islands. The local tectonic plate (in the case of the Hawaii hotspot, the Pacific Plate) slowly slides over the hotspot, carrying its volcanoes with it without affecting the plume. Over hundreds of thousands of years, the magma supply for the volcano is slowly cut off, eventually going extinct. No longer active enough to overpower erosion, the volcano slowly sinks beneath the waves, becoming a seamount once again. As the cycle continues, a new volcanic center manifests, and a volcanic island arises anew. The process continues until the mantle plume itself collapses.[1]

text: This cycle of growth and dormancy strings together volcanoes over millions of years, leaving a trail of volcanic islands and seamounts across the ocean floor. According to Wilson's theory, the Hawaiian volcanoes should be progressively older and increasingly eroded the further they are from the hotspot, and this is easily observable; the oldest rock in the main Hawaiian islands, that of Kauaʻi, is about 5.5 million years old and deeply eroded, while the rock on Hawaiʻi island is a comparatively young 0.7 million years of age or less, with new lava constantly erupting at Kīlauea, the hotspot's present center.[1][5] Another consequence of his theory is that the chain's length and orientation serves to record the direction and speed of the Pacific Plate's movement. A major feature of the Hawaiian trail is a sudden 60° bend at a 40- to 50-million-year-old section of its length, and according to Wilson's theory, this is evidence of a major change in plate direction, one that would have initiated subduction along much of the Pacific Plate's western boundary.[6] This part of the theory has recently been challenged, and the bend might be attributed to the movement of the hotspot itself.[7]

text: Geophysicists believe that hotspots originate at one of two major boundaries deep in the Earth, either a shallow interface in the lower mantle between an upper convecting layer and a lower non-convecting layer, or a deeper D'' ("D double-prime") layer, approximately 200 kilometres (120 mi) thick and immediately above the core-mantle boundary.[8] A mantle plume would initiate at the interface when the warmer lower layer heats a portion of the cooler upper layer. This heated, buoyant, and less-viscous portion of the upper layer would become less dense due to thermal expansion, and rise towards the surface as a Rayleigh-Taylor instability.[8] When the mantle plume reaches the base of the lithosphere, the plume heats it and produces melt. This magma then makes its way to the surface, where it is erupted as lava.[9]

text: Arguments for the validity of the hotspot theory generally center on the steady age progression of the Hawaiian islands and nearby features:[10] a similar bend in the trail of the Macdonald hotspot, the Austral–Marshall Islands seamount chain, located just south;[11] other Pacific hotspots following the same age-progressed trend from southeast to northwest in fixed relative positions;[12][13] and seismologic studies of Hawaii which show increased temperatures at the core–mantle boundary, evidencing a mantle plume.[14]

text: Shallow hotspot hypothesis[edit]

text: Another hypothesis is that melting anomalies form as a result of lithospheric extension, which allows pre-existing melt to rise to the surface. These melting anomalies are normally called "hotspots", but under the shallow-source hypothesis the mantle underlying them is not anomalously hot. In the case of the Emperor-Hawaiian seamount chain, the Pacific plate boundary system was very different at ~ 80 Ma, when the Emperor seamount chain began to form. There is evidence that the chain started on a spreading ridge (the Pacific-Kula Ridge) that has now been subducted at the Aleutian trench.[15] The locus of melt extraction may have migrated off the ridge and into the plate interior, leaving a trail of volcanism behind it. This migration may have occurred because this part of the plate was extending in order to accommodate intraplate stress. Thus, a long-lived region of melt escape could have been sustained. Supporters of this hypothesis argue that the wavespeed anomalies seen in seismic tomographic studies cannot be reliably interpreted as hot upwellings originating in the lower mantle.[16][17]

text: Moving hotspot theory[edit]

text: The most heavily challenged element of Wilson's theory is whether or not hotspots are indeed fixed relative to the overlying tectonic plates. Drill samples, collected by scientists as far back as 1963, suggest that the hotspot may have drifted over time, at the relatively rapid pace of about 4 centimeters (1.6 in) per year during the late Cretaceous and early Paleogene eras (81-47 Mya);[18] in comparison, the Mid-Atlantic Ridge spreads at a rate of 2.5 cm (1.0 in) per year.[1] In 1987, a study published by Peter Molnar and Joann Stock found that the hotspot does move relative to the Atlantic Ocean; however, they interpreted this as the result of the relative motions of the North American and Pacific plates rather than that of the hotspot itself.[19]

text: In 2001 the Ocean Drilling Program (since merged into the Integrated Ocean Drilling Program), an international research effort to study the world's seafloors, funded a two-month expedition aboard the research vessel JOIDES Resolution to collect lava samples from four submerged Emperor seamounts. The project drilled Detroit, Nintoku, and Koko seamounts, all of which are in the far northwest end of the chain, the oldest section.[20][21] These lava samples were then tested in 2003, suggested a mobile Hawaiian hotspot and a shift in its motion as the cause of the bend.[7][22] Lead scientist John Tarduno told National Geographic:

text: The Hawaii bend was used as a classic example of how a large plate can change motion quickly. You can find a diagram of the Hawaii – Emperor bend entered into just about every introductory geological textbook out there. It really is something that catches your eye."[22]

text: Despite the large shift, the change in direction was never recorded by magnetic declinations, fracture zone orientations or plate reconstructions; nor could a continental collision have occurred fast enough to produce such a pronounced bend in the chain.[23] To test whether or not the bend was a result of a change in direction of the Pacific Plate, scientists analyzed the lava samples' geochemistry to determine where and when they formed. Age was determined by the radiometric dating of radioactive isotopes of potassium and argon. Researchers estimated that the volcanoes formed during a period 81 million to 45 million years ago. Tarduno and his team determined where the volcanoes formed by analyzing the rock for the magnetic mineral magnetite. While hot lava from a volcanic eruption cools, tiny grains within the magnetite align with the Earth's magnetic field, and lock in place once the rock solidifies. Researchers were able to verify the latitudes at which the volcanoes formed by measuring the grains' orientation within the magnetite. Paleomagnetists concluded that the Hawaiian hotspot had drifted southward sometime in its history, and that, 47 million years ago, the hotspot's southward motion greatly slowed, perhaps even stopping entirely.[20][22]

text: History of study[edit]

text: Ancient Hawaiian[edit]

text: The possibility that the Hawaiian islands became older as one moved to the northwest was suspected by ancient Hawaiians long before Europeans arrived. During their voyages, seafaring Hawaiians noticed differences in erosion, soil formation, and vegetation, allowing them to deduce that the islands to the northwest (Niʻihau and Kauaʻi) were older than those to the southeast (Maui and Hawaii).[1] The idea was handed down the generations through the legend of Pele, the fiery Hawaiian Goddess of Volcanoes.

text: Pele was born to the female spirit Haumea, or Hina, who, like all Hawaiian gods and goddesses, descended from the supreme beings, Papa, or Earth Mother, and Wakea, or Sky Father.[24]:63[25] According to the myth, Pele originally lived on Kauai, when her older sister Nāmaka, the Goddess of the Sea, attacked her for seducing her husband. Pele fled southeast to the island of Oahu. When forced by Nāmaka to flee again, Pele moved southeast to Maui and finally to Hawaii, where she still lives in the Halemaumau Crater at the summit of Kīlauea. There she was safe, because the slopes of the volcano are so high that even Nāmaka's mighty waves could not reach her. Pele's mythical flight, which alludes to an eternal struggle between volcanic islands and ocean waves, is consistent with geologic evidence about the ages of the islands decreasing to the southeast.[1][18]

text: Modern studies[edit]

text: Three of the earliest recorded observers of the volcanoes were the Scottish scientists Archibald Menzies in 1794,[26] James Macrae in 1825,[27] and David Douglas in 1834. Just reaching the summits proved daunting: Menzies took three attempts to ascend Mauna Loa, and Douglas died on the slopes of Mauna Kea. The United States Exploring Expedition spent several months studying the islands in 1840–1841.[28] American geologist James Dwight Dana was on that expedition, as was Lieutenant Charles Wilkes, who spent most of the time leading a team of hundreds that hauled a pendulum to the summit of Mauna Loa to measure gravity. Dana stayed with missionary Titus Coan, who would provide decades of first-hand observations.[29] Dana published a short paper in 1852.[30]

text: Dana remained interested in the origin of the Hawaiian Islands, and directed a more in-depth study in 1880 and 1881. He confirmed that the islands' age increased with their distance from the southeastern-most island by observing differences in their degree of erosion. He also suggested that many other island chains in the Pacific showed a similar general increase in age from southeast to northwest. Dana concluded that the Hawaiian chain consisted of two volcanic strands, located along distinct but parallel curving pathways. He coined the terms "Loa" and "Kea" for the two prominent trends. The Kea trend includes the volcanoes of Kīlauea, Mauna Kea, Kohala, Haleakalā, and West Maui. The Loa trend includes Lōiʻhi, Mauna Loa, Hualālai, Kahoʻolawe, Lānaʻi, and West Molokaʻi. Dana proposed that the alignment of the Hawaiian Islands reflected localized volcanic activity along a major fissure zone. Dana's "great fissure" theory served as the working hypothesis for subsequent studies until the mid-20th century.[23]

text: Dana's work was followed up by geologist C. E. Dutton's 1884 expedition, who refined and expanded Dana's ideas. Most notably, Dutton established that the island of Hawaii actually harbored five volcanoes, whereas Dana counted three. This is because Dana had originally regarded Kīlauea as a flank vent of Mauna Loa, and Kohala as part of Mauna Kea. Dutton also refined others of Dana's observations, and is credited with the naming of 'a'ā and pāhoehoe-type lavas, although Dana had noted a distinction. Stimulated by Dutton's expedition, Dana returned in 1887, and published many accounts of his expedition in the American Journal of Science. In 1890 he published the most detailed manuscript of its day, and remained the definitive guide to Hawaiian volcanism for decades. 1909 saw the publication of two large volumes which extensively quoted from earlier works now out of circulation.[31]:154–155

text: In 1912 geologist Thomas Jaggar founded the Hawaiian Volcano Observatory. The facility was taken over in 1919 by the National Oceanic and Atmospheric Administration and in 1924 by the United States Geological Survey (USGS), which marked the start of continuous volcano observation on Hawaii island. The next century was a period of thorough investigation, marked by contributions from many top scientists. The first complete evolutionary model was first formulated in 1946, by USGS geologist and hydrologist Harold T. Stearns. Since that time, advances have enabled the study of previously limited areas of observation (e.g. improved rock dating methods and submarine volcanic stages).[31]:157[32]

text: In the 1970s, the Hawaiian seafloor was mapped using ship-based sonar. Computed SYNBAPS (Synthetic Bathymetric Profiling System)[33] data filled holes between the ship-based sonar bathymetric measurements.[19][34] From 1994 to 1998[35] the Japan Agency for Marine-Earth Science and Technology (JAMSTEC) mapped Hawaii in detail and studied its ocean floor, making it one of the world's best-studied marine features. The JAMSTEC project, a collaboration with USGS and other agencies, utilized manned submersibles, remotely operated underwater vehicles, dredge samples, and core samples.[36] The Simrad EM300 multibeam side-scanning sonar system collected bathymetry and backscatter data.[35]

text: Characteristics[edit]

text: Position[edit]

text: The Hawaii hotspot has been imaged through seismic tomography, and is estimated to be 500–600 km (310–370 mi) wide.[37][38] Tomographic images show a thin low-velocity zone extending to a depth of 1,500 km (930 mi), connecting with a large low-velocity zone extending from a depth of 2,000 km (1,200 mi) to the core-mantle boundary. These low seismic velocity zones often indicate hotter and more buoyant mantle material, consistent with a plume originating in the lower mantle and a pond of plume material in the upper mantle. The low-velocity zone associated with the source of the plume is north of Hawaiʻi, showing that the plume is tilted to a certain degree, deflected toward the south by mantle flow.[39] Uranium decay-series disequilibria data has shown that the actively flowing region of the melt zone is 220 ± 40 km (137 ± 25 mi) km wide at its base and 280 ± 40 km (174 ± 25 mi) at the upper mantle upwelling, consistent with tomographic measurements.[40]

text: Temperature[edit]

text: Indirect studies found that the magma chamber is located about 90–100 kilometers (56–62 mi) underground, which matches the estimated depth of the Cretaceous Period rock in the oceanic lithosphere; this may indicate that the lithosphere acts as a lid on melting by arresting the magma's ascent. The magma's original temperature was found in two ways, by testing garnet's melting point in lava and by adjusting the lava for olivine deterioration. Both USGS tests seem to confirm the temperature at about 1,500 °C (2,730 °F); in comparison, the estimated temperature for mid-ocean ridge basalt is about 1,325 °C (2,417 °F).[41]

text: The surface heat flow anomaly around the Hawaiian Swell is only of the order of 10 mW/m2,[42][43] far less than the continental United States range of 25 to 150 mW/m2.[44] This is unexpected for the classic model of a hot, buoyant plume in the mantle. However, it has been shown that other plumes display highly variable surface heat fluxes and that this variability may be due to variable hydrothermal fluid flow in the Earth's crust above the hotspots. This fluid flow advectively removes heat from the crust, and the measured conductive heat flow is therefore lower than the true total surface heat flux.[43] The low heat across the Hawaiian Swell indicates that it is not supported by a buoyant crust or upper lithosphere, but is rather propped up by the upwelling hot (and therefore less-dense) mantle plume that causes the surface to rise[42] through a mechanism known as "dynamic topography".

text: Movement[edit]

text: Hawaiian volcanoes drift northwest from the hotspot at a rate of about 5–10 centimeters (2.0–3.9 in) a year.[18] The hotspot has migrated south by about 800 kilometers (497 mi) relative to the Emperor chain.[23] Paleomagnetic studies support this conclusion based on changes in Earth's magnetic field, a picture of which was engrained in the rocks at the time of their solidification,[45] showing that these seamounts formed at higher latitudes than present-day Hawaii. Prior to the bend, the hotspot migrated an estimated 7 centimeters (2.8 in) per year; the rate of movement changed at the time of the bend to about 9 centimeters (3.5 in) per year.[23] The Ocean Drilling Program provided most of the current knowledge about the drift. The 2001[46] expedition drilled six seamounts and tested the samples to determine their original latitude, and thus the characteristics and speed of the hotspot's drift pattern in total.[47]

text: Each successive volcano spends less time actively attached to the plume. The large difference between the youngest and oldest lavas between Emperor and Hawaiian volcanoes indicates that the hotspot's velocity is increasing. For example, Kohala, the oldest volcano on Hawaii island, is one million years old and last erupted 120,000 years ago, a period of just under 900,000 years; whereas one of the oldest, Detroit Seamount, experienced 18 million or more years of volcanic activity.[21]

text: The oldest volcano in the chain, Meiji Seamount, perched on the edge of the Aleutian Trench, formed 85 million years ago.[48] At its current velocity, the seamount will be destroyed within a few million years, as the Pacific Plate slides under the Eurasian Plate. It is unknown whether the seamount chain has been subducting under the Eurasian Plate, and whether the hotspot is older than Meiji Seamount, as any older seamounts have since been destroyed by the plate margin. It is also possible that a collision near the Aleutian Trench had changed the velocity of the Pacific Plate, explaining the hotspot chain's bend; the relationship between these features is still being investigated.[23][49]

text: Magma[edit]

text: The composition of the volcanoes' magma has changed significantly according to analysis of the strontium–niobium–palladium elemental ratios. The Emperor Seamounts were active for at least 46 million years, with the oldest lava dated to the Cretaceous Period, followed by another 39 million years of activity along the Hawaiian segment of the chain, totaling 85 million years. Data demonstrate vertical variability in the amount of strontium present in both the alkalic (early stages) and tholeitic (later stages) lavas. The systematic increase slows drastically at the time of the bend.[48]

text: Almost all magma created by the hotspot is igneous basalt; the volcanoes are constructed almost entirely of this or the similar in composition but coarser-grained gabbro and diabase. Other igneous rocks such as nephelinite are present in small quantities; these occur often on the older volcanoes, most prominently Detroit Seamount.[48] Most eruptions are runny because basaltic magma is less viscous than magmas characteristic of more explosive eruptions such as the andesitic magmas that produce spectacular and dangerous eruptions around Pacific Basin margins.[7] Volcanoes fall into several eruptive categories. Hawaiian volcanoes are called "Hawaiian-type". Hawaiian lava spills out of craters and forms long streams of glowing molten rock, flowing down the slope, covering acres of land and replacing ocean with new land.[50]

text: Eruption frequency and scale[edit]

text: There is significant evidence that lava flow rates have been increasing. Over the last six million years they have been far higher than ever before, at over 0.095 km3 (0.023 cu mi) per year. The average for the last million years is even higher, at about 0.21 km3 (0.050 cu mi). In comparison, the average production rate at a mid-ocean ridge is about 0.02 km3 (0.0048 cu mi) for every 1,000 kilometers (621 mi) of ridge. The rate along the Emperor seamount chain averaged about 0.01 cubic kilometers (0.0024 cu mi) per year. The rate was almost zero for the initial five million or so years in the hotspot's life. The average lava production rate along the Hawaiian chain has been greater, at 0.017 km3 (0.0041 cu mi) per year.[23] In total, the hotspot has produced an estimated 750,000 cubic kilometers (180,000 cu mi) of lava, enough to cover California with a layer about 1.5 kilometers (1 mi) thick.[5][18][51][52][53]

text: The distance between individual volcanoes has shrunk. Although volcanoes have been drifting north faster and spending less time active, the far greater modern eruptive volume of the hotspot has generated more closely spaced volcanoes, and many of them overlap, forming such superstructures as Hawaiʻi island and the ancient Maui Nui. Meanwhile, many of the volcanoes in the Emperor seamounts are separated by 100 kilometers (62 mi) or even as much as 200 kilometers (124 mi).[52][53]

text: Topography and geoid[edit]

text: A detailed topographic analysis of the Hawaiian – Emperor seamount chain reveals the hotspot as the center of a topographic high, and that elevation falls with distance from the hotspot. The most rapid decrease in elevation and the highest ratio between the topography and geoid height are over the southeastern part of the chain, falling with distance from the hotspot, particularly at the intersection of the Molokai and Murray fracture zones. The most likely explanation is that the region between the two zones is more susceptible to reheating than most of the chain. Another possible explanation is that the hotspot strength swells and subsides over time.[34]

text: In 1953, Robert S. Dietz and his colleagues first identified the swell behavior. It was suggested that the cause was mantle upwelling. Later work pointed to tectonic uplift, caused by reheating within the lower lithosphere. However, normal seismic activity beneath the swell, as well as lack of detected heat flow, caused scientists to suggest dynamic topography as the cause, in which the motion of the hot and buoyant mantle plume supports the high surface topography around the islands.[42] Understanding the Hawaiian swell has important implications for hotspot study, island formation, and inner Earth.[34]

text: Volcanoes[edit]

text: Over its 85 million year history, the Hawaii hotspot has created at least 129 volcanoes, more than 123 of which are extinct volcanoes, seamounts, and atolls, four of which are active volcanoes, and two of which are dormant volcanoes.[21][47][54] They can be organized into three general categories: the Hawaiian archipelago, which comprises most of the U.S. state of Hawaii and is the location of all modern volcanic activity; the Northwestern Hawaiian Islands, which consist of coral atolls, extinct islands, and atoll islands; and the Emperor Seamounts, all of which have since eroded and subsided to the sea and become seamounts and guyots (flat-topped seamounts).[55]

text: Volcanic characteristics[edit]

text: Hawaiian volcanoes are characterized by frequent rift eruptions, their large size (thousands of cubic kilometers in volume), and their rough, decentralized shape. Rift zones are a prominent feature on these volcanoes, and account for their seemingly random volcanic structure.[56] The tallest mountain in the Hawaii chain, Mauna Kea, rises 4,205 meters (13,796 ft) above mean sea level. Measured from its base on the seafloor, it is the world's tallest mountain, at 10,203 meters (33,474 ft); Mount Everest rises 8,848 meters (29,029 ft) above sea level.[57] Hawaii is surrounded by a myriad of seamounts; however, they were found to be unconnected to the hotspot and its volcanism.[36] Kīlauea has erupted continuously since 1983 through Puʻu ʻŌʻō, a minor volcanic cone, which has become an attraction for volcanologists and tourists alike.[58]

text: Landslides[edit]

text: The Hawaiian islands are carpeted by a large number of landslides sourced from volcanic collapse. Bathymetric mapping has revealed at least 70 large landslides on the island flanks over 20 km (12 mi) in length, and the longest are 200 km (120 mi) long and over 5,000 km3 (1,200 cu mi) in volume. These debris flows can be sorted into two broad categories: slumps, mass movement over slopes which slowly flatten their originators, and more catastrophic debris avalanches, which fragment volcanic slopes and scatter volcanic debris past their slopes. These slides have caused massive tsunamis and earthquakes, fractured volcanic massifs, and scattered debris hundreds of miles away from their source.[59]

text: Slumps tend to be deeply rooted in their originators, moving rock up to 10 km (6 mi) deep inside the volcano. Forced forward by the mass of newly ejected volcanic material, slumps may creep forward slowly, or surge forward in spasms that have caused the largest of Hawaii's historical earthquakes, in 1868 and 1975. Debris avalanches, meanwhile, are thinner and longer, and are defined by volcanic amphitheaters at their head and hummocky terrain at their base. Rapidly moving avalanches carried 10 km (6 mi) blocks tens of kilometers away, disturbing the local water column and causing a tsunami. Evidence of these events exists in the form of marine deposits high on the slopes of many Hawaiian volcanoes,[59] and has marred the slopes of several Emperor seamounts, such as Daikakuji Guyot and Detroit Seamount.[21]

text: Evolution and construction[edit]

text: Hawaiian volcanoes follow a well-established life cycle of growth and erosion. After a new volcano forms, its lava output gradually increases. Height and activity both peak when the volcano is around 500,000 years old and then rapidly decline. Eventually it goes dormant, and eventually extinct. Erosion then weathers the volcano until it again becomes a seamount.[55]

text: This life cycle consists of several stages. The first stage is the submarine preshield stage, currently represented solely by Lōʻihi Seamount. During this stage, the volcano builds height through increasingly frequent eruptions. The sea's pressure prevents explosive eruptions. The cold water quickly solidifies the lava, producing the pillow lava that is typical of underwater volcanic activity.[55][60]

text: As the seamount slowly grows, it goes through the shield stages. It forms many mature features, such as a caldera, while submerged. The summit eventually breaches the surface, and the lava and ocean water "battle" for control as the volcano enters the explosive subphase. This stage of development is exemplified by explosive steam vents. This stage produces mostly volcanic ash, a result of the waves dampening the lava.[55] This conflict between lava and sea influences Hawaiian mythology.[24]:8–11

text: The volcano enters the subaerial subphase once it is tall enough to escape the water. Now the volcano puts on 95% of its above-water height over roughly 500,000 years. Thereafter eruptions become much less explosive. The lava released in this stage often includes both pāhoehoe and ʻaʻā, and the currently active Hawaiian volcanoes, Mauna Loa and Kīlauea, are in this phase. Hawaiian lava is often runny, blocky, slow, and relatively easy to predict; the USGS tracks where it is most likely to run, and maintains a tourist site for viewing the lava.[55][61]

text: After the subaerial phase the volcano enters a series of postshield stages involving subsidence and erosion, becoming an atoll and eventually a seamount. Once the Pacific Plate moves it out of the 20 °C (68 °F) tropics, the reef mostly dies away, and the extinct volcano becomes one of an estimated 10,000 barren seamounts worldwide.[55][62] Every Emperor seamount is a dead volcano.


document_title: List of Back to the Future characters

question_text: who played marty's daughter in back to the future 2

question_tokens: who played marty 's daughter in back to the future 2

root

text: List of Back to the Future characters

text: Main characters[edit]

text: Marty McFly[edit]

text: Martin Seamus "Marty" McFly (portrayed by Michael J. Fox in the films and voiced by David Kaufman in the animated series and AJ LoCascio in Back to the Future: The Game) is the son of George McFly and Lorraine Baines McFly. Marty travels between the past and the future, encountering his ancestors and descendants. Marty and his friend Doc Brown help restore the space-time continuum while encountering Biff Tannen (or members of the Tannen clan) at various points in time.

tag: p

text: Emmett "Doc" Brown[edit]

text: Doctor Emmett Lathrop "Doc" Brown (portrayed by Christopher Lloyd in the films and Back to the Future: The Game, and voiced by Dan Castellaneta in the animated series) is the inventor of the DeLorean time machine. At various points in time, Doc helps Marty restore the space-time continuum and reverse the changes that were caused by time travel.

text: In 2008, the character was selected by film magazine Empire as one of The 100 Greatest Movie Characters of All Time, ranking at #20.[1]

text: Biff Tannen[edit]

text: Biff Howard Tannen (portrayed by Thomas F. Wilson in the films and animated series and voiced by Kid Beyond in Back to the Future: The Game) is the main antagonist of the first 2 films and a local bully who harassed George McFly and has once altered history in the second film. He comes from a long line of bullies in Hill Valley, most of whom harassed members of the McFly family. Biff is also a descendant of Buford Tannen (also portrayed by Wilson), who is one of Hill Valley's outlaws during the 1880s.

text: McFly family[edit]

text: George McFly[edit]

text: George Douglas McFly (portrayed by Crispin Glover in Back to the Future and by Jeffrey Weissman in Back to the Future Part II and Back to the Future Part III and voiced by Michael X. Sommers in Back to the Future: The Game) is the father of Marty, Linda and Dave from the union with his wife Lorraine Baines McFly. Although he is one of the main characters in the first movie, George only makes cameos in Back to the Future Part II and Back to the Future Part III.

text: In the first film, George is portrayed as weak and the main target of Biff Tannen's bullying. The novelization of the film expounds on George's history of weakness, describing two incidents in which he is unable to stand up for himself. In 1955, in contrast with Marty, George did not have any friends for support and was targeted not only by Biff and his gang but also other kids in school. He has a penchant for science fiction, and writes some of his own but never allows himself to share them with anyone due to his fear of rejection. In 1955, with Marty's help, he gets the courage to stand up to Biff, knocking him unconscious. As a result, he and Lorraine fall in love and George becomes popular in school for defeating Biff in a fight. In the new future, they are both happily married with George working as a college professor and being a successful writer who orders Biff around. In the alternate timeline in Part II, George was murdered by Biff in 1973.

text: George's character was greatly reduced in the sequels, and the role was recast to Jeffrey Weissman.[2] Weissman wore prosthetics to resemble Glover and imitated Glover's rendering of McFly, and his scenes were spliced with shots of Glover from Back to the Future.[3] The result was so convincing that many people were fooled by it.[3] Glover did not appreciate this, and sued. The lawsuit resulted in the adoption of stricter rules by the Screen Actors Guild to prevent this situation from occurring again.[3]

text: Lorraine Baines-McFly[edit]

text: Lorraine Baines-McFly (portrayed by Lea Thompson and voiced by Aimee Miles in Back to the Future: The Game) is the wife of George McFly and the mother of Marty, Linda and Dave. She is the eldest daughter of Sam (George DiCenzo) and Stella (Frances Lee McCain) Baines, and sister of Milton (Jason Hervey), Sally (Maia Brewton), Toby, and Joey.

text: In Back to the Future, Lorraine is initially portrayed in 1985 as middle-aged and unhappy. After Marty changes the timeline, she is shown to be fit and happily married to George in 1985. In Part II, she is still happily married to George in 2015, but in the dystopian alternate 1985 timeline she is widowed and married to Biff.

text: Dave McFly[edit]

text: David "Dave" McFly (portrayed by Marc McClure) is the eldest child of George and Lorraine McFly. In 1985 before Marty went to 1955, Dave works at Burger King, but in the post-time travel 1985 he wears a suit as a nondescript white-collar worker for an accounting firm. In a deleted scene from Part II, the alternate 1985 timeline shows that Dave is an alcoholic and a gambling addict following George's death and Lorraine's second marriage to Biff.

text: Linda McFly[edit]

text: Linda McFly (portrayed by Wendie Jo Sperber) is the middle child and only daughter of George and Lorraine McFly. In 1985 before Marty went to 1955, Linda is having boy trouble and it is unknown if she is in college or has a job. In 1985 after Marty went to 1955, Linda works in a boutique and has gained the attention of many boys.

text: Seamus and Maggie McFly[edit]

text: Seamus and Maggie McFly (portrayed by Michael J. Fox and Lea Thompson) are Irish immigrants and the paternal great-great-grandparents of Marty McFly. In Part III, Marty is befriended by Seamus and Maggie. While Maggie does not trust the "strange young man", Seamus has a familiar feeling about him and believes that helping him is the right thing to do. They have a son named William (Marty's great-grandfather). Much like his descendants, Seamus is harassed by a member of the Tannen family, Buford Tannen.

text: Maggie McFly is played by Lea Thompson, who also plays Marty's mother Lorraine, even though Maggie is not an ancestor of Lorraine; in a DVD commentary track for Part III, Bob Gale states that the creative team considered it important to include Thompson in the film, and he imagines that McFly men are simply "genetically predisposed" to be attracted to women who look like her.

text: Marty (Jr.) and Marlene McFly[edit]

text: Marty (Jr.) and Marlene McFly (both portrayed by Michael J. Fox) are Marty McFly and Jennifer Parker's future fraternal twin son and daughter in Part II.

text: Originally Marty (Jr.) was to be arrested for joining a robbery initiated by Griff and his gang. Marlene attempted to help Marty Jr. break out of jail but failed and was sentenced to 20 years in a woman's prison. Doc and Marty prevented the event from ever happening.

text: Brown family[edit]

text: Clara Clayton[edit]

text: Clara Clayton (portrayed by Mary Steenburgen in both Back to the Future Part III and the animated series) is the wife of Doc Brown and mother of Jules and Verne Brown.

text: Clara moved to Hill Valley and originally died in an accident when her wagon plummeted into Shonash Ravine, which was renamed Clayton Ravine in her memory. The animated series reveals that Clara, along with the rest of the family, moves to the early 1990s and lives in a farmhouse outside of Hill Valley. She then becomes a teacher at Hill Valley Elementary School.

text: Jules and Verne Brown[edit]

text: Jules Eratosthenes Brown and Verne Newton Brown (portrayed by Todd Cameron Brown and Daniel Evans in Back to the Future Part III and voiced by Josh Keaton and Troy Davidson in the animated series) are the two children of Doc Brown and his wife, Clara, who named them after their favorite author Jules Verne.

text: The characters had minor, non-speaking roles in Back to the Future Part III but were further developed in the animated series. Jules, an introvert, mostly imitates his father's interests and mannerisms while Verne appears to be more outgoing and extroverted. Several plot points of the animated series revolve around either Jules or Verne altering history and the steps necessary to correct the damage.

text: Copernicus[edit]

text: Copernicus is Doc's dog from 1955. Like his other dogs, Copernicus was used in many of Doc's experiments. When Copernicus died, he was replaced by Einstein.

text: Einstein[edit]

text: Einstein (portrayed by Tiger in the first film and Freddie in the other two and voiced by Danny Mann in the animated series) is Doc Brown's pet Catalan sheepdog. He later becomes one of the main characters in the animated series as the Brown family's dog.

text: In the first film, Doc successfully tests his time machine by placing Einstein in it and sending him one minute into the future. In the animated series, Einstein becomes anthropomorphic and smarter, helping Doc with his inventions for traveling to the past and the future.

text: Tannen family[edit]

text: Irving "Kid" Tannen[edit]

text: Kid Tannen is Biff's father who only appears in the Back to the Future game. Kid is a gangster who runs a local speakeasy in the 1930s Hill Valley. He, like the rest of the Tannen family, bullies the McFly family forcing Marty's grandfather Arthur to do his accounting. Kid is brought down with the help of Marty, a young version of Doc, and Arthur McFly. He later marries Edna Strickland and reforms from his criminal ways with her help.

text: Buford "Mad Dog" Tannen[edit]

text: Buford Tannen (portrayed by Thomas F. Wilson in Back to the Future Part III) is the main antagonist of the third film. He is the great-grandfather of Biff Tannen and the local town outlaw in 1885 Hill Valley. He was nicknamed "Mad Dog" by a newspaper reporter, due to his violent temper and propensity for drooling, a nickname Tannen greatly despises. Buford is cruel, homicidal, rude, and emotionally unstable. He displays a need for control and is brought down to childlike tantrums when he is humiliated or makes mistakes, whether it be something that happens to him or something he says or does. He is often accompanied by his gang (played by Christopher Wynne, Sean Sullivan and Mike Watson), and developed a feud with Marshal James Strickland and his deputies.

text: Griff[edit]

text: Griff (portrayed by Thomas F. Wilson in both Back to the Future Part II and in the animated series) is a grandson of Biff. He is part of a gang that also consists of "Data", "Spike", and "Whitey" (portrayed by Ricky Dean Logan, Darlene Vogel, and Jason Scott Lee).

text: In the animated series, Griff makes a brief cameo appearance in the episode "Solar Sailors" where his grandson, Ziff (also voiced by Wilson), is detained after he attempts to sabotage Marta McFly's space cruiser due to his hatred towards her family.

text: Griff's last name is never mentioned in the movies, which means he could either be the son of Biff's son Biff Jr, or the son of Biff's daughter, Tiffaney. However, in the animated series, Ziff refers that both he and Griff are Tannens.

text: Biff Tannen, Jr.[edit]

text: In the animated series, Biff Jr. is the son of Biff Tannen. Like his father and paternal relatives, he likes to bully and steal from children around him including Jules and Verne Brown with whom he developed a feud. In addition, Biff Jr. delights vandalizing other people's properties. Biff Jr. lives with his father with whom he has an abusive relationship. He is voiced by Benji Gregory.

text: Strickland family[edit]

text: Gerald Strickland[edit]

text: Gerald Strickland[4] (portrayed by James Tolkan) is the strict principal of Hill Valley High School. He is the grandson of Chief Marshal James Strickland of Hill Valley 1885.

text: There is a reference from Verne Brown that there is another Strickland who works at Hill Valley Elementary School as its vice principal.[episode needed]

text: James Strickland[edit]

text: James Strickland (portrayed by James Tolkan in Back to the Future Part III) is the chief marshal of Hill Valley in 1885 and the grandfather of Mr. Strickland. He also has an unnamed son (portrayed by Kaleb Henley), who will become Gerald Strickland's father.

text: Edna Strickland[edit]

text: Edna Strickland, in Back to the Future: The Game, is the sister of Gerald Strickland. She is somewhat nicer than her brother, but still set in her ways towards upholding strong morals and abolishing crime and laziness. After Marty alters her original timeline, Edna marries Kid Tannen who becomes the father of Biff Tannen.

text: Other characters[edit]

text: Jennifer Parker[edit]

text: Jennifer Jane Parker is the girlfriend (and, in 2015 in Back to the Future Part II, the wife) of Marty McFly.

text: The character was played by Claudia Wells in Back to the Future. However, Wells was not available to film the sequels for personal reasons, and the role was recast to Elisabeth Shue although Wells reprised her role as Jennifer in Back to the Future: The Game as a punk rock version of her character. Consequently, the opening scene of Back to the Future Part II was re-shot with Shue taking Wells' place, rather than using the ending of Back to the Future. In the spin-off Back to the Future: the Animated Series, Jennifer was voiced by Cathy Cavadini.

text: In 1985, Jennifer attends Hill Valley High School, along with her boyfriend Marty. In the animated series, Jennifer is enrolled to Hill Valley College with Marty after graduating high school and working part-time as a tutor. She lives with her family on a ranch, the deed to which was owned by Biff Tannen, after one of his ancestors forced Jennifer's great-great-grandfather to sign it over by holding Jennifer's great-great-grandmother hostage. In the episode "A Friend in Deed", Marty travels back in time to 1875 and sabotages the deal with help from Jules and Verne.[5]

text: In the future witnessed in Back to the Future Part II, Jennifer and Marty had two children, Marlene and Marty Jr. (both played by Michael J. Fox)

text: Douglas J. Needles[edit]

text: Douglas J. Needles (portrayed by Flea in Back to the Future Part II and Back to the Future Part III) is an acquaintance of Marty McFly and Jennifer Parker from Hill Valley High School. Like his school's alumnus, Biff Tannen, Needles also has his own gang (portrayed by Christopher Wynne, J.J. Cohen, and Ricky Dean Logan) and develops a rivalry with Marty. Needles often goads Marty into doing reckless things such as a street race that leads Marty to crash into a Rolls Royce and an illegal transaction which results in his firing in 2015.

text: Goldie Wilson[edit]

text: Goldie Wilson (played by Donald Fullilove in part 1) is a young man working at Lou's Cafe in 1955 who goes on to become the first black Mayor of Hill Valley in the 1980s. A campaign poster shows the name Goldie in quotation marks, suggesting Goldie is a nickname, presumably in reference to his gold tooth. He would also have a grandson, Goldie Wilson III (also played by Fullilove) in Part II, who works as a car salesman.

text: Match, Skinhead, and 3-D[edit]

text: Match (portrayed by Billy Zane), Skinhead (portrayed by Jeffrey Jay Cohen), and 3-D (portrayed by Casey Siemaszko) are the three high school boys who make up Biff Tannen's gang in 1955. Their nicknames are only given in the films' novels, screenplays, and credits. Only one of their real names is mentioned in the movies – Biff refers to Skinhead as Joey in one of the 1955 scenes in Back to the Future Part II, while outside of the "Enchantment Under the Sea" dance.

text: In the alternate 1985, the three work in Biff's casino as his bodyguards. Each gets his nickname from a distinctive character trait. Match often has a match sticking out of his mouth; Skinhead has very short, close-cropped hair; 3-D is always wearing a pair of anaglyphic 3-D glasses (a reference to the 3-D movies that were popular in the 1950s).


document_title: International distress frequency

question_text: what is the coast guard emergency hf frequency

text: International distress frequency

text: History[edit]

text: For much of the 20th century, 500 kHz was the primary international distress frequency. Its use has been phased out in favor of the Global Maritime Distress Safety System.

text: Use of some distress frequencies is permitted for calling other stations to establish contact, whereupon the stations move to another frequency. Such channels are known as distress, safety and calling frequencies.[1]

text: Satellite processing from all 121.5 or 243 MHz locators has been discontinued. Since February 1, 2009, the U.S. Coast Guard only monitors distress signals from emergency position indicating radio beacons that broadcast using digital 406 MHz signals.[2] Digital 406 MHz models became the only ones approved for use in both commercial and recreational watercraft worldwide on January 1, 2007.[3]

text: Current frequencies[edit]

text: International distress frequencies, currently in use are:

text:
2182 kHz for medium range maritime voice use. The US Coast Guard has said "beginning August 1st, 2013 the Coast Guard would no longer monitor 2182 kHz",[4] as have many other coast guard services.
Several HF maritime voice frequencies exist for long-distance distress calls:[5]

4.125 MHz
6.215 MHz
8.291 MHz
12.290 MHz
16.420 MHz

121.5 MHz is the civilian aircraft emergency frequency or International Air Distress frequency. It is used by civilian distress radiobeacons; however, the Cospas-Sarsat system no longer monitors the frequency.
243 MHz for NATO military aircraft emergency frequencies
Marine VHF radio Channel 16 (156.8 MHz) for short range maritime use
406 MHz to 406.1 MHz is used by the Cospas-Sarsat international satellite-based search and rescue (SAR) distress alert detection and information distribution system
462.675 MHz is a UHF mobile distress and road information calling frequency allocated to the General Mobile Radio Service and used throughout Alaska and Canada for emergency communications; formerly called Orange Dot in the 1960s, "GMRS 675" or Channel 6 on mobile radios today. Its bandwidth can vary between 12.5, 25 and 50 kHz, and is also allocated to Ch. 20 on 22-channel FRS/GMRS "blister pack" radios. It can have a repeater input frequency of 467.675 MHz, and a tone squelch of 141.3 Hz.

tag: ul

text: Digital selective calling frequencies[edit]

text: Several maritime frequencies are used for digital selective calling (DSC), and they are also monitored for DSC distress signals:[5][6]

text:
2.1875 MHz
4.2075 MHz
6.312 MHz
8.4145 MHz
12.577 MHz
16.8045 MHz
156.525 MHz, Marine VHF radio Channel 70

text: Amateur radio frequencies[edit]

text: Emergency Centre of Activity (ECOA) frequencies informally established by the International Amateur Radio Union regional organizations (frequencies shown in kHz):

text:
Region 1[7]
Europe, Africa
Region 2[8]
The Americas
Region 3[9]
Asia

3760
3750 or 3985
3600

7110
7060, 7240 or 7275
7110

14300
14300
14300

18160
18160
18160

21360
21360
21360

tag: table

text:
Emergency/Disaster Relief Interoperation Voice Channels of the amateur radio Global ALE High Frequency Network:[10]

3791.0 kHz USB
7185.5 kHz USB
10145.5 kHz USB
14346.0 kHz USB
18117.5 kHz USB
21432.5 kHz USB
24932.0 kHz USB
28312.5 kHz USB

Citizens band (CB) radio (not available in all countries)

Emergency channels 9 (27.065 MHz AM) and 19 (27.185 MHz AM)


document_title: Big Ten Conference Men's Basketball Tournament

question_text: when was the last time purdue won the big ten tournament

text: Host[edit]

text: The Big Ten Men's Basketball tournaments have been held at neutral sites every year. The first four tournaments were held at United Center in Chicago, Illinois. Beginning in 2002, the tournament alternated between United Center and Conseco Fieldhouse (later known as Bankers Life Fieldhouse) in Indianapolis, Indiana. In 2008, the tournament began a five-year residence in Indianapolis.[1]

text: On June 5, 2011, the Big Ten announced that the tournament would revert to alternating between Indianapolis and Chicago. The 2013 and 2015 tournaments were played at United Center in Chicago and the 2014 and 2016 tournaments were played at Bankers Life Fieldhouse in Indianapolis.[2]

text: The 2017 Tournament was held at Verizon Center in Washington, D.C.[3][4] The 2018 Tournament was held at Madison Square Garden in New York and held a week earlier than usual due to the Big East Tournament, ending on March 4, 2018, one week before Selection Sunday.[5][6][7] The 2019 through 2022 Tournaments will return to alternating between United Center in Chicago and Bankers Life Fieldhouse in Indianapolis.[8]

text: Vacated results[edit]

text: Due to various rulings against participating programs, some of the results of the Big Ten Tournament have been vacated or voided. Here is a compiled list of sanctions imposed that have affected the results and records of the tournament since its inception. The information in this article does not include results of the teams in which records were vacated.

text:
Because of the Minnesota academic scandal, the NCAA has vacated the postseason tournament records for the Minnesota basketball team from the 1993–94 season through the 1998–99 season.[9] Minnesota had a record of 2–1 in the 1998 Tournament and went 0–1 in 1999.
Because of the Michigan basketball scandal, the NCAA vacated the records for the Michigan basketball team from the 1995–96 season through the 1998–99 season, including the 1998 and 1999 Big Ten Tournaments.[10] Michigan had won the Tournament championship in 1998 with a 3–0 record, and had a record of 1–1 in 1999.
The NCAA has vacated the NCAA records for the Ohio State basketball team from the 1998–99 season through the 2001–02 season.[11] Ohio State had a record of 1–1 in the 1999 Tournament, went 0–1 in 2000 and 2001, and had won the championship in 2002.

text: Results and records[edit]

text: Results by year[edit]

text:
Year
Champion
Seed
Score
Runner-up
Seed
Most Valuable Player
Site

1998
Michigan (vacated) [note 1]
4
76–67
Purdue
3
Robert Traylor, Michigan [note 1]
United Center, Chicago

1999
Michigan State
1
67–50
Illinois
11
Mateen Cleaves, Michigan State
United Center, Chicago

2000
Michigan State
2
76–61
Illinois
4
Morris Peterson, Michigan State
United Center, Chicago

2001
Iowa
6
63–61
Indiana
4
Reggie Evans, Iowa
United Center, Chicago

2002
Ohio State (vacated) [note 2]
2
81–64
Iowa
9
Boban Savovic, Ohio State [note 2]
Conseco Fieldhouse, Indianapolis

2003
Illinois
2
72–59
Ohio State
8
Brian Cook, Illinois
United Center, Chicago

2004
Wisconsin
2
70–53
Illinois
1
Devin Harris, Wisconsin
Conseco Fieldhouse, Indianapolis

2005
Illinois
1
54–43
Wisconsin
2
James Augustine, Illinois
United Center, Chicago

2006
Iowa
2
67–60
Ohio State
1
Jeff Horner, Iowa
Conseco Fieldhouse, Indianapolis

2007
Ohio State
1
66–49
Wisconsin
2
Mike Conley Jr., Ohio State
United Center, Chicago

2008
Wisconsin
1
61–48
Illinois
10
Marcus Landry, Wisconsin
Conseco Fieldhouse, Indianapolis

2009
Purdue
3
65–61
Ohio State
5
Robbie Hummel, Purdue
Conseco Fieldhouse, Indianapolis

2010
Ohio State
1
90–61
Minnesota
6
Evan Turner, Ohio State
Conseco Fieldhouse, Indianapolis

2011
Ohio State
1
71–60
Penn State
6
Jared Sullinger, Ohio State
Conseco Fieldhouse, Indianapolis

2012
Michigan State
1
68–64
Ohio State
3
Draymond Green, Michigan State
Conseco Fieldhouse, Indianapolis

2013
Ohio State
2
50–43
Wisconsin
4
Aaron Craft, Ohio State
United Center, Chicago

2014
Michigan State
3
69–55
Michigan
1
Branden Dawson, Michigan State
Bankers Life Fieldhouse, Indianapolis

2015
Wisconsin
1
80–69OT
Michigan State
3
Frank Kaminsky, Wisconsin
United Center, Chicago

2016
Michigan State
2
66–62
Purdue
4
Denzel Valentine, Michigan State
Bankers Life Fieldhouse, Indianapolis

2017
Michigan
8
71–56
Wisconsin
2
Derrick Walton, Michigan
Verizon Center, Washington, D.C.

2018
Michigan
5
75–66
Purdue
3
Moritz Wagner, Michigan
Madison Square Garden, New York City

2019

United Center, Chicago

2020

Bankers Life Fieldhouse, Indianapolis

2021

United Center, Chicago

2022

Bankers Life Fieldhouse, Indianapolis

text: Most conference tournament championships[edit]

text:
School
Titles
Years

Michigan State
5
1999, 2000, 2012, 2014, 2016

Ohio State^
4
2007, 2010, 2011, 2013

Wisconsin
3
2004, 2008, 2015

Illinois
2
2003, 2005

Iowa
2
2001, 2006

Michigan*
2
2017, 2018

Purdue
1
2009

Minnesota
0

Indiana
0

Penn State
0

Northwestern
0

Nebraska
0

Maryland
0

Rutgers
0

text:
* 1998 championship vacated by Michigan.
^ 2002 championship vacated by Ohio State.

text: Most consecutive championships[edit]

text: 2 – Michigan State (1999, 2000), Ohio State (2010, 2011), Michigan (2017, 2018)

text: Records all-time by team[edit]

text:
School
Record
Winning pct
Championships
Runners-up

Ohio State
26–14[note 2]
.650
4
4

Michigan State
29–16
.644
5
1

Illinois
27–19
.587
2
4

Wisconsin
24–18
.571
3
3

Michigan
22–17[note 1]
.564
2
1

Iowa
16–19
.457
2
1

Rutgers
3–4
.429
0
0

Minnesota
14–19[note 3]
.424
0
1

Purdue
14–20
.412
1
3

Penn State
14–21
.400
0
1

Indiana
12–21
.364
0
1

Maryland
2–4
.333
0
0

Nebraska
3–7
.300
0
0

Northwestern
9–21
.300
0
0

text: Records all-time by seed[edit]

text:
Seed
Record
Winning pct
Championships
Runners-up

1
34–12
.739
8
3

2
26–12[note 2]
.684
5*
2

3
20–17[note 2]
.541
2
4

4
14–19[note 1]
.424
0*
3

5
15–19
.441
1
1

6
28–18[note 3]
.609
1
2

7
15–20
.429
0
0

8
15–19[note 3]
.441
1
1

9
9–20
.310
0
1

10
10–19[note 1]
.345
0
1

11
7–20
.259
0
1

12
3–6
.333
0
0

13
2–3
.400
0
0

14
3–4
.429
0
0

text: * Does not include vacated wins by Michigan (1998) and Ohio State (2002)

text: Records by coaches[edit]

text: Through 2018 tournament

text:
Coach
School
Record
Winning pct.
Championships

Thad Matta
Ohio State
23–9
.719
4

Bill Self
Illinois
5–2
.714
1

Steve Alford
Iowa
13–6
.684
2

John Beilein
Michigan
19–9
.679
2

Lon Kruger
Illinois
6–3
.667
0

Tom Izzo
Michigan State
29–16
.644
5

Bo Ryan
Wisconsin
17–11
.607
3

Bruce Weber
Illinois
12–8
.600
1

Mike Davis
Indiana
7–6
.538
0

Tubby Smith
Minnesota
7–6
.538
0

Matt Painter
Purdue
11–12
.478
1

Pat Chambers
Penn State
5–7
.417
0

Ed DeChellis
Penn State
5–8
.385
0

Bill Carmody
Northwestern
5–13
.278
0

text: Note: Current coaches at school in bold. Minimum of five wins.[12]

text: Notes[edit]

text:
^ Jump up to: a b c d e Due to NCAA sanctions, Michigan has vacated the records from the 1992 Final Four, the 1992–93, 1995–96, 1996–97, 1997–98, and 1998–99 seasons. See above section Vacated results
^ Jump up to: a b c d e Due to NCAA sanctions, Ohio State has vacated the records of 34 games in 1998–99, 16 games in 1999–00 and the entire 2000–01 and 2001–02 seasons. See above section Vacated results
^ Jump up to: a b c Due to NCAA sanctions, Minnesota has vacated the records from the 1993–94, 1994–95, 1995–96, 1996–97, 1997–98, and 1998–99 seasons. See above section Vacated results

tag: ol

text: Television coverage[edit]


document_title: Macduff (Macbeth)

question_text: at the end of act v who will be crowned as new king of scotland

text: Macduff (Macbeth)

text: Origin[edit]

text: The overall plot that would serve as the basis for Macbeth is first seen in the writings of two chroniclers of Scottish history, John of Fordun, whose prose Chronica Gentis Scotorum was begun about 1363, and Andrew of Wyntoun's Scots verse Orygynale Cronykil of Scotland, written no earlier than 1420. These served as the basis for the account given in Holinshed's Chronicles (1587), on whose narratives of King Duff and King Duncan Shakespeare in part based Macbeth.

text: Historically, Duff was a 10th century King of Alba. In John of Fordun's work, the reign of Duff is portrayed as having suffered from pervasive witchcraft. The Orygynale Cronykil suggests that Duff was murdered. Due to the Irish use of tanistry, Duff's immediate descendants did not become rulers of Alba, and instead became mormaers of Fife. Their clan – the Clan MacDuff – remained the most powerful family in Fife in the medieval ages.[1].

text: In Holinshed's narrative, attributes of King Duff are transposed onto the MacDuff mormaer from Macbeth's era. Macduff first appears in Holinshed's narrative of King Duncan after Macbeth has killed the latter and reigned as King of Scotland for 10 years. When Macbeth calls upon his nobles to contribute to the construction of Dunsinane castle, Macduff avoids the summons, arousing Macbeth's suspicions. Macduff leaves Scotland for England to prod Duncan's son, Malcolm III of Scotland, into taking the Scottish throne by force. Meanwhile, Macbeth murders Macduff's family. Malcolm, Macduff, and the English forces march on Macbeth, and Macduff kills him.[2] Shakespeare follows Holinshed's account of Macduff closely, with his only deviations being Macduff's discovery of Duncan's body in 2.3, and Macduff's brief conference with Ross in 2.4.

text: The ruins of Macduff's Castle lie in East Wemyss cemetery.

text: Role in the play[edit]

text: Macduff first speaks in the play in act 2, scene 3 to the drunken porter to report to his duty of awaking King Duncan when he is sleeping for the night at Macbeth's castle. When he discovers the corpse of King Duncan (murdered by Macbeth, but it looks like nearby guards are guilty since Macbeth—at the prodding of Lady Macbeth—put his knife by them and smeared them with Duncan's blood), he raises an alarm, informing the castle that the king has been murdered. Macduff begins to suspect Macbeth of regicide when Macbeth says, "O, yet I do repent me of my fury / That I did kill them" (2.3.124–125). Interestingly, Macduff's name does not appear in this scene; rather, Banquo refers to him as "Dear Duff" (2.3.105).

text: In 2.4 Macbeth has left for Scone, the ancient royal city where Scottish kings were crowned. Macduff, meanwhile, meets with Ross and an Old Man. He reveals that he will not be attending the coronation of Macbeth and will instead return to his home in Fife. However, Macduff flees to England to join Malcolm, the slain King Duncan's elder son, and convinces him to return to Scotland and claim the throne.

text: Macbeth, meanwhile, visits the Three Witches again after the spectre of Banquo appears at the royal banquet. The Witches warn Macbeth to "beware Macduff, beware the Thane of Fife" (4.1.81–82). Furthermore, they inform him that, "The power of man, for none of woman born / Shall harm Macbeth" (4.1.91–92). Macbeth, fearing for his position as King of Scotland, learns soon afterward that Macduff has fled to England to try to raise an army against him and orders the deaths of Macduff's wife, children and relatives. Macduff, who is still in England, learns of his family's deaths through Ross, another Scottish thane. He joins Malcolm, and they return to Scotland with their English allies to face Macbeth at Dunsinane Castle.

text: After Macbeth slays the young Siward, Macduff charges into the main castle and confronts Macbeth. Although Macbeth believes that he cannot be killed by any man born of a woman, he soon learns that Macduff was "from his mother's womb / Untimely ripped" (5.10.15–16). The two fight, and Macduff slays Macbeth offstage. Macduff ultimately presents Macbeth's head to Malcolm, hailing him as king and calling on the other thanes to declare their allegiance with him (5.11.20–25).

text: Analysis[edit]

text: Macduff as a foil to Macbeth[edit]

text: As a supporting character, Macduff serves as a foil to Macbeth; his integrity directly contrasts with Macbeth's moral perversion.[3] In an exchange between the Scottish thane Lennox and another lord, Lennox talks of Macduff’s flight to England and refers to him as "some holy angel" (3.6.46) who "may soon return to this our suffering country / Under a hand accursed" (3.6.48–49). The play positions the characters of Macduff and Macbeth as holy versus evil

text: The contrast between Macduff and Macbeth is accentuated by their approaches to death. Macduff, hearing of his family’s death, reacts with a tortured grief. His words, "But I must also feel it as a man" (4.3.223), indicate a capacity for emotional sensitivity. While Macbeth and Lady Macbeth insist that manhood implies a denial of feeling (1.7.45–57), Macduff insists that emotional depth and sensitivity are part of what it means to be a man. This interpretation is supported by Macduff’s reaction upon his discovery of Duncan’s corpse and the echo of Macduff’s words when Macbeth responds to the news of Lady Macbeth’s death. Macduff struggles to find the words to express his rage and anguish, crying, "O horror, horror, horror" (2.3.59). In some stage interpretations, Macduff’s character transitions from a state of shock to one of frenzied alarm.[4] This contrasts starkly with Macbeth’s famous response to the announcement of his wife’s death: "She should have died hereafter / There would have been a time for such a word / Tomorrow, and tomorrow, and tomorrow" (5.5.17–19). Macbeth’s words seem to express a brutal indifference–she would have died anyway–and perhaps even suggest that he has lost the capacity to feel.

text: Macduff as a moral figure[edit]

text: Although Macduff comes to represent a type of "goodness" in the dark world of Macbeth, Shakespeare also allows for some instability in his character. This becomes most evident in 4.3 when Macduff joins Malcolm in England. In this scene, the play has moved from the tumult in Scotland to England. In the exchange between the two Scotsmen, Malcolm is clearly in control and forces Macduff to examine and reconcile with himself his own moral code. In a moment of dramatic irony, Macduff begins the conversation urging Malcolm to fight for Scotland rather than to grieve, not knowing that Malcolm has already arranged for English military support (4.3.134–136). Malcolm manipulates Macduff, questioning his loyalty, facilitating his emotional responses, and testing to see how much Macduff’s, and perhaps the audience’s, morality can ultimately be compromised. Malcolm portrays Macbeth as a tyrant, but he positions himself, too, as someone morally repulsive.[4] He describes his own voluptuousness–the bottomless "cistern of [his] lust" (4.3.64)–and "staunchless avarice" (4.3.79). Macduff must decide whether he can accept Malcolm as an alternative to Macbeth. But Macduff cannot accept Malcolm's presentation of himself "Fit to Govern! No, not to live." (4.3.103–104). So Malcolm recognises he can trust Macduff and comes clean "abjure[d] / The taints and blames I laid upon myself, / For strangers to my nature"(4.3.125–127). This shows that rather than speaking truthfully about himself, Malcolm was simply testing Macduff to see where Macduff's loyalties were.

text: Macduff may also be read as a precursor for ethical philosophy.[5] Macduff's flight from Scotland is a "spiritual reawakening", with spirituality based around the truth, regardless of what it may be. Macduff constantly re-examines his values. In deciding to leave his family, Macduff deserts those values and pays bitterly for it. Macduff echoes sentiments of writers such as Plato and the later Thomas Hobbes, who claim that morality may only be judged to the extent that a person takes responsibility for his or her actions. Thus, because he accepts the burden of his decision to leave his family for political exploration, Macduff's actions can be justified.[5]

text: Macbeth and the fantasy of female power[edit]

text: It has been argued that the play Macbeth wrestles with the relationship between male vulnerability and feminine influence. The play, on this interpretation, explores the fantasy of a female or maternal power as well as the desire of an escape from this influence.[6] Femaleness is to be feared and reviled, and to a certain extent, the play works to excise femininity and restore autonomous male or paternal power. However, the play also exposes the impossibility of the fantasy of absolute masculinity.