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Large igneous province

Topic: Earth

 From HandWiki - Reading time: 18 min
Short description: Huge regional accumulation of igneous rocks
Only a few of the largest large igneous provinces appear (coloured dark purple) on this geologic map, which depicts crustal geologic provinces as seen in seismic refraction data.

A large igneous province (LIP) is an extremely large accumulation of igneous rocks, including intrusive (sills, dikes) and extrusive (lava flows, tephra deposits), arising when magma travels through the crust towards the surface. The formation of LIPs is variously attributed to mantle plumes or to processes associated with divergent plate tectonics.[1] The formation of some of the LIPs in the past 500 million years coincide in time with mass extinctions and rapid climatic changes, which has led to numerous hypotheses about causal relationships. LIPs are fundamentally different from any other currently active volcanoes or volcanic systems.

Definition

In 1992 researchers first used the term large igneous province to describe very large accumulations—areas greater than 100,000 square kilometers (approximately the area of Iceland)—of mafic igneous rocks that were erupted or emplaced at depth within an extremely short geological time interval: a few million years or less.[2] Mafic basalt sea floors and other geological products of 'normal' plate tectonics were not included in the definition.[3]

Types

The definition of LIP has been expanded and refined, and is still a work in progress. LIP is now frequently also used to describe voluminous areas of, not just mafic, but all types of igneous rocks. Sub-categorization of LIPs into large volcanic provinces (LVP) and large plutonic provinces (LPP), and including rocks produced by normal plate tectonic processes, have been proposed, but these modifications are not generally accepted.[4]

Some LIPs are geographically intact, such as the basaltic Deccan Traps in India, while others have been fragmented and separated by plate movements, like the Central Atlantic Magmatic Province (CAMP)—parts of which are found in Brazil, eastern North America, and north-western Africa.[5]

Motivations for study of LIPs

Large igneous provinces (LIPs) are created during short-lived igneous events resulting in relatively rapid and high-volume accumulations of volcanic and intrusive igneous rock. These events warrant study because:

  • The possible links to mass extinctions and global environmental and climatic changes. Michael Rampino and Richard Stothers (1988) cited eleven distinct flood-basalt episodes – occurring in the past 250 million years – which created volcanic provinces and oceanic plateaus and coincided with mass extinctions.[6] This theme has developed into a broad field of research, bridging geoscience disciplines such as biostratigraphy, volcanology, metamorphic petrology, and Earth System Modelling.
  • The study of LIPs has economic implications. Some workers associate them with trapped hydrocarbons.[citation needed] They are associated with economic concentrations of copper–nickel and iron.[7] They are also associated with formation of major mineral provinces including Platinum-Group Element (PGE) Deposits and, in the silicic LIPs, silver and gold deposits.[3] Titanium and vanadium deposits are also found in association with LIPs.[8]
  • LIPs in the geological record have marked major changes in the hydrosphere and atmosphere, leading to major climate shifts and maybe mass extinctions of species.[3] Some of these changes were related to rapid release of greenhouse gases from the crust to the atmosphere. Thus the LIP-triggered changes may be used as cases to understand current and future environmental changes.
  • Plate tectonic theory explains topography using interactions between the tectonic plates, as influenced by viscous stresses created by flow within the underlying mantle. Since the mantle is extremely viscous, the mantle flow rate varies in pulses which are reflected in the lithosphere by small amplitude, long wavelength undulations. Understanding how the interaction between mantle flow and lithosphere elevation influences formation of LIPs is important to gaining insights into past mantle dynamics.[9]
  • LIPs have played a major role in continental breakup, continental formation, new crustal additions from the upper mantle, and supercontinent cycles.[9]

Large igneous province formation

Three Devils Grade in Moses Coulee, Washington is part of the Columbia River Basalt Group LIP.

Earth has an outer shell made of a number of discrete, moving tectonic plates floating on a solid convective mantle above a liquid core. The mantle's flow is driven by the descent of cold tectonic plates during subduction and the complementary ascent of plumes of hot material from lower levels. The surface of the Earth reflects stretching, thickening and bending of the tectonic plates as they interact.[10]

Ocean-plate creation at upwellings, spreading and subduction are well accepted fundamentals of plate tectonics, with the upwelling of hot mantle materials and the sinking of the cooler ocean plates driving the mantle convection. In this model, tectonic plates diverge at mid-ocean ridges, where hot mantle rock flows upward to fill the space. Plate-tectonic processes account for the vast majority of Earth's volcanism.[11]

Beyond the effects of convectively driven motion, deep processes have other influences on the surface topography. The convective circulation drives up-wellings and down-wellings in Earth's mantle that are reflected in local surface levels. Hot mantle materials rising up in a plume can spread out radially beneath the tectonic plate causing regions of uplift.[10] These ascending plumes play an important role in LIP formation.

Formation characteristics

When created, LIPs often have an areal extent of a few million km2 and volumes on the order of 1 million km3. In most cases, the majority of a basaltic LIP's volume is emplaced in less than 1 million years. One of the conundra of such LIPs' origins is to understand how enormous volumes of basaltic magma are formed and erupted over such short time scales, with effusion rates up to an order of magnitude greater than mid-ocean ridge basalts.

Formation theories

The source of many or all LIPs are variously attributed to mantle plumes, to processes associated with plate tectonics or to meteorite impacts.

Plume formation of LIPs

Although most volcanic activity on Earth is associated with subduction zones or mid-oceanic ridges, there are significant regions of long-lived, extensive volcanism, known as hotspots, which are only indirectly related to plate tectonics. The Hawaiian–Emperor seamount chain, located on the Pacific Plate, is one example, tracing millions of years of relative motion as the plate moves over the Hawaii hotspot. Numerous hotspots of varying size and age have been identified across the world. These hotspots move slowly with respect to one another, but move an order of magnitude more quickly with respect to tectonic plates, providing evidence that they are not directly linked to tectonic plates.[11]

The origin of hotspots remains controversial. Hotspots that reach the Earth's surface may have three distinct origins. The deepest probably originate from the boundary between the lower mantle and the core; roughly 15–20% have characteristics such as presence of a linear chain of sea mounts with increasing ages, LIPs at the point of origin of the track, low shear wave velocity indicating high temperatures below the current location of the track, and ratios of 3He to 4He which are judged consistent with a deep origin. Others such as the Pitcairn, Samoan and Tahitian hotspots appear to originate at the top of large, transient, hot lava domes (termed superswells) in the mantle. The remainder appear to originate in the upper mantle and have been suggested to result from the breakup of subducting lithosphere.[12]

Recent imaging of the region below known hotspots (for example, Yellowstone and Hawaii) using seismic-wave tomography has produced mounting evidence that supports relatively narrow, deep-origin, convective plumes that are limited in region compared to the large-scale plate tectonic circulation in which they are imbedded. Images reveal continuous but tortuous vertical paths with varying quantities of hotter material, even at depths where crystallographic transformations are predicted to occur.[13][clarification needed]

Plate-related stress formation of LIPs

A major alternative to the plume model is a model in which ruptures are caused by plate-related stresses that fractured the lithosphere, allowing melt to reach the surface from shallow heterogeneous sources. The high volumes of molten material that form the LIPs is postulated to be caused by convection in the upper mantle, which is secondary to the convection driving tectonic plate motion.[14]

Early formed reservoir outpourings

It has been proposed that geochemical evidence supports an early-formed reservoir that survived in the Earth's mantle for about 4.5 billion years. Molten material is postulated to have originated from this reservoir, contributing the Baffin Island flood basalt about 60 million years ago. Basalts from the Ontong Java plateau show similar isotopic and trace element signatures proposed for the early-Earth reservoir.[15]

Meteorite-induced formation

Seven pairs of hotspots and LIPs located on opposite sides of the earth have been noted; analyses indicate this coincident antipodal location is highly unlikely to be random. The hotspot pairs include a large igneous province with continental volcanism opposite an oceanic hotspot. Oceanic impacts of large meteorites are expected to have high efficiency in converting energy into seismic waves. These waves would propagate around the world and reconverge close to the antipodal position; small variations are expected as the seismic velocity varies depending upon the route characteristics along which the waves propagate. As the waves focus on the antipodal position, they put the crust at the focal point under significant stress and are proposed to rupture it, creating antipodal pairs. When the meteorite impacts a continent, the lower efficiency of kinetic energy conversion into seismic energy is not expected to create an antipodal hotspot.[14]

A second impact-related model of hotspot and LIP formation has been suggested in which minor hotspot volcanism was generated at large-body impact sites and flood basalt volcanism was triggered antipodally by focused seismic energy. This model has been challenged because impacts are generally considered seismically too inefficient, and the Deccan Traps of India were not antipodal to, and began erupting several Myr before, the end-Cretaceous Chicxulub impact in Mexico. In addition, no clear example of impact-induced volcanism, unrelated to melt sheets, has been confirmed at any known terrestrial crater.[14]

Classification

In 1992, Coffin and Eldholm initially defined the term "large igneous province" (LIP) as representing a variety of mafic igneous provinces with areal extent greater than 100,000 km2 that represented "massive crustal emplacements of predominantly mafic (magnesium- and iron-rich) extrusive and intrusive rock, and originated via processes other than 'normal' seafloor spreading."[16][17][18] That original definition included continental flood basalts, oceanic plateaus, large dike swarms (the eroded roots of a volcanic province), and volcanic rifted margins. Most of these LIPs consist of basalt, but some contain large volumes of associated rhyolite (e.g. the Columbia River Basalt Group in the western United States); the rhyolite is typically very dry compared to island arc rhyolites, with much higher eruption temperatures (850 °C to 1000 °C) than normal rhyolites.

Since 1992 the definition of 'LIP' has been expanded and refined, and remains a work in progress. Some new definitions of the term 'LIP' include large granitic provinces such as those found in the Andes Mountains of South America and in western North America. Comprehensive taxonomies have been developed to focus technical discussions.

In 2008, Bryan and Ernst refined the definition to narrow it somewhat: "Large Igneous Provinces are magmatic provinces with areal extents >1×105 km2, igneous volumes >1×105 km3 and maximum lifespans of ~50 Myr that have intraplate tectonic settings or geochemical affinities, and are characterised by igneous pulse(s) of short duration (~1–5 Myr), during which a large proportion (>75%) of the total igneous volume has been emplaced. They are dominantly mafic, but also can have significant ultramafic and silicic components, and some are dominated by silicic magmatism." This definition places emphasis on the high magma emplacement rate characteristics of the LIP event and excludes seamounts, seamount groups, submarine ridges and anomalous seafloor crust.[19]

'LIP' is now frequently used to also describe voluminous areas of, not just mafic, but all types of igneous rocks. Sub-categorization of LIPs into Large Volcanic Provinces (LVP) and Large Plutonic Provinces (LPP), and including rocks produced by 'normal' plate tectonic processes, has been proposed. Further, the minimum threshold to be included as a LIP has been lowered to 50,000 km2.[4] The working taxonomy, focused heavily on geochemistry, which will be used to structure examples below, is:

  • Large igneous provinces (LIP)
    • Large volcanic provinces (LVP)
      • Large rhyolitic provinces (LRPs)
      • Large andesitic provinces (LAPs)
      • Large basaltic provinces (LBPs): oceanic, or continental flood basalts
      • Large basaltic–rhyolitic provinces (LBRPs)
    • Large plutonic provinces (LPP)
      • Large granitic provinces (LGP)
      • Large mafic plutonic provinces
Illustration showing a vertical dike and a horizontal sill.

Aerally extensive dike swarms, sill provinces, and large layered ultramafic intrusions are indicators of LIPs, even when other evidence is not now observable. The upper basalt layers of older LIPs may have been removed by erosion or deformed by tectonic plate collisions occurring after the layer is formed. This is especially likely for earlier periods such as the Paleozoic and Proterozoic.[19]

Giant dyke swarms having lengths over 300 km[20] are a common record of severely eroded LIPs. Both radial and linear dyke swarm configurations exist. Radial swarms with an areal extent over 2,000 km and linear swarms extending over 1,000 km are known. The linear dyke swarms often have a high proportion of dykes relative to country rocks, particularly when the width of the linear field is less than 100 km. The dykes have a typical width of 20–100 m, although ultramafic dykes with widths greater than 1 km have been reported.[19]

Dykes are typically sub-vertical to vertical. When upward flowing (dyke-forming) magma encounters horizontal boundaries or weaknesses, such as between layers in a sedimentary deposit, the magma can flow horizontally creating a sill. Some sill provinces have areal extents >1000 km.[19]

Correlations with LIP formation

Correlation with hot-spots

The early volcanic activity of major hotspots, postulated to result from deep mantle plumes, is frequently accompanied by flood basalts. These flood basalt eruptions have resulted in large accumulations of basaltic lavas emplaced at a rate greatly exceeding that seen in contemporary volcanic processes. Continental rifting commonly follows flood basalt volcanism. Flood basalt provinces may also occur as a consequence of the initial hot-spot activity in ocean basins as well as on continents. It is possible to track the hot spot back to the flood basalts of a large igneous province; the table below correlates large igneous provinces with the track of a specific hot spot.[21][22]

Province Region Hotspot Reference
Columbia River Basalt Northwestern US Yellowstone hotspot [21][23]
Ethiopia-Yemen Flood Basalts Ethiopia, Yemen [21]
North Atlantic Igneous Province Northern Canada, Greenland, the Faeroe Islands, Norway , Ireland and Scotland Iceland hotspot [21]
Deccan Traps India Réunion hotspot [21]
Rajmahal Traps India Ninety East Ridge [24][25]
Kerguelen Plateau Indian Ocean Kerguelen hotspot [24]
Ontong Java Plateau Pacific Ocean Louisville hotspot [21][22]
Paraná and Etendeka traps Brazil –Namibia Tristan hotspot [21]
Karoo-Ferrar Province South Africa, Antarctica, Australia & New Zealand Marion Island [21]
Caribbean large igneous province Caribbean-Colombian oceanic plateau Galápagos hotspot [26][27]
Mackenzie Large Igneous Province Canadian Shield Mackenzie hotspot [28]

Relationship to extinction events

Eruptions or emplacements of LIPs appear to have, in some cases, occurred simultaneously with oceanic anoxic events and extinction events. The most important examples are the Deccan Traps (Cretaceous–Paleogene extinction event), the Karoo-Ferrar (Pliensbachian-Toarcian extinction), the Central Atlantic Magmatic Province (Triassic-Jurassic extinction event), and the Siberian traps (Permian-Triassic extinction event).

Several mechanisms are proposed to explain the association of LIPs with extinction events. The eruption of basaltic LIPs onto the earth's surface releases large volumes of sulfate gas, which forms sulfuric acid in the atmosphere; this absorbs heat and causes substantial cooling (e.g., the Laki eruption in Iceland, 1783). Oceanic LIPs can reduce oxygen in seawater by either direct oxidation reactions with metals in hydrothermal fluids or by causing algal blooms that consume large amounts of oxygen.[29]

Ore deposits

Large igneous provinces are associated with a handful of ore deposit types including:

Examples

There are a number of well-documented examples of large igneous provinces identified by geological research.

Province Region Age (million years) Area (million km2) Volume (million km3) Also known as or includes Reference
Agulhas Plateau Southwest Indian Ocean, South Atlantic Ocean, Southern Ocean 140–95 0.3 1.2 Southeast African LIP
Mozambique Ridge, Northeast Georgia Rise, Maud Rise, Astrid Ridge 		[30]
Columbia River Basalt Northwestern US 17–6 0.16 0.175 [23][31]
Ethiopia-Yemen Flood Basalts Yemen, Ethiopia 31–25 0.6 0.35 Ethiopia [31]
North Atlantic Igneous Province Northern Canada, Greenland, the Faeroe Islands, Norway, Ireland, and Scotland 62–55 1.3 6.6

Jameson Land Thulean Plateau

[31]
Deccan Traps India 66 0.5–0.8 0.5–1.0 [31]
Madagascar 88 [32]
Rajmahal Traps India 116 [24][25]
Ontong Java Plateau Pacific Ocean c. 122 1.86 8.4 Manihiki Plateau and Hikurangi Plateau [31]
High Arctic Large Igneous Province Svalbard, Franz Josef Land, Sverdrup Basin, Amerasian Basin, and northern Greenland 130-60 > 1.0 [33]
Paraná and Etendeka traps Brazil, Namibia 134–129 1.5 > 1 Equatorial Atlantic Magmatic Province

Brazilian Highlands

[31]
Karoo-Ferrar Province South Africa, Antarctica, Australia, and New Zealand 183–180 0.15–2 0.3 [31]
Central Atlantic magmatic province Northern South America, Northwest Africa, Iberia, Eastern North America 199–197 11 2.5 (2.0–3.0) [34][35]
Siberian Traps Russia 250 1.5–3.9 0.9–2.0 [31]
Emeishan Traps Southwestern China 253–250 0.25 c. 0.3 [31]
Warakurna large igneous province Australia 1078–1073 1.5 Eastern Pilbara [36]

Large rhyolitic provinces (LRPs)

These LIPs are composed dominantly of felsic materials. Examples include:

  • Whitsunday
  • Sierra Madre Occidental (Mexico)
  • Malani
  • Chon Aike (Argentina)
  • Gawler (Australia)

Large andesitic provinces (LAPs)

These LIPs are comprised dominantly of andesitic materials. Examples include:

  • Island arcs such as Indonesia and Japan
  • Active continental margins such as the Andes and the Cascades
  • Continental collision zones such as the Anatolia-Iran zone

Large basaltic provinces (LBPs)

This subcategory includes most of the provinces included in the original LIP classifications. It is composed of continental flood basalts, oceanic flood basalts, and diffuse provinces.

Continental flood basalts

Oceanic flood basalts/ oceanic plateaus

Large basaltic–rhyolitic provinces (LBRPs)

  • Snake River Plain – Oregon High Lava Plains[37]
  • Dongargarh, India[37]

Large plutonic provinces (LPP)

  • Equatorial Atlantic Magmatic Province

Large granitic provinces (LGP)

  • Patagonia
  • Peru–Chile Batholith
  • Coast Range Batholith (NW US)

Other large plutonic provinces

  • Parts of Central Atlantic Magmatic Province (eastern United States and Canada, northern South America, northwest Africa)

Silicic-dominated Large Igneous Province (SLIP)

These are by definition formed by large volumes of magma (≥100000 km3) emplaced over a relatively short time, some millions of years. They have occurred throughout geological history of the earth, in both intraplate and plate margin examples. There are only a few recognised SLIP in the world, including:[38]

  • Gawler Range Volcanics (GRV) and the co-magmatic Hiltaba Suite (HS), Gawler Ranges, South Australia. These form a mesoproterozoic SLIP.

Related structures

Volcanic rifted margins

Extension thins the crust. Magma reaches the surface through radiating sills and dikes, forming basalt flows, as well as deep and shallow magma chambers below the surface. The crust gradually thins due to thermal subsidence, and originally horizontal basalt flows are rotated to become seaward dipping reflectors.

Volcanic rifted margins are found on the boundary of large igneous provinces. Volcanic margins form when rifting is accompanied by significant mantle melting, with volcanism occurring before and/or during continental breakup. Volcanic rifted margins are characterized by: a transitional crust composed of basaltic igneous rocks, including lava flows, sills, dikes, and gabbros, high volume basalt flows, seaward-dipping reflector sequences (SDRS) of basalt flows that were rotated during the early stages of breakup, limited passive-margin subsidence during and after breakup, and the presence of a lower crust with anomalously high seismic P-wave velocities in lower crustal bodies (LCBs), indicative of lower temperature, dense media.

Example of volcanic margins include:

  • The Yemen margin
  • The East Australian margin
  • The West Indian margin
  • The Hatton–Rockal margin
  • The US East Coast
  • The mid-Norwegian margin
  • The Brazilian margins
  • The Namibian margin

Dike swarms

Map of the Mackenzie dike swarm in Canada

A dike swarm is a large geological structure consisting of a major group of parallel, linear, or radially oriented dikes intruded within continental crust. They consist of several to hundreds of dikes emplaced more or less contemporaneously during a single intrusive event, and are magmatic and stratigraphic. Such dike swarms are the roots of a volcanic province. Examples include:

  • Mackenzie dike swarm (Canadian Shield)
  • Long Range dikes (Newfoundland and Labrador, Canada)
  • Mistassini dike swarm (western Quebec, Canada)
  • Matachewan dike swarm (northern Ontario, Canada)
  • Sorachi Plateau and Belt (Hokkaido, Japan)
  • Rio Ceará-Mirim dike swarm (Borborema Province, NE Brazil)
  • Uralian dike swarm (Russia)[39]

Sills

A series of related sills that were formed essentially contemporaneously (within several million years) from related dikes comprise a LIP if their area is sufficiently large. Examples include:

  • Winagami sill complex (northwestern Alberta, Canada)
  • Bushveld Igneous Complex (South Africa) with an area of over 66,000 km2 (25,000 sq mi), and a thickness reaching 9 kilometres (5.6 mi) thick.

See also

References

  1. ↑ Foulger, G. R. (2010). Plates vs. Plumes: A Geological Controversy. Wiley-Blackwell. ISBN 978-1-4051-6148-0. http://www.wiley.com/WileyCDA/WileyTitle/productCd-1405161485.html. 
  2. ↑ Coffin, M; Eldholm, O (1992). "Volcanism and continental break-up: a global compilation of large igneous provinces". in Storey, B.C.. Magmatism and the Causes of Continental Breakup. Special Publications. 68. London: Geological Society of London. 17–30. doi:10.1144/GSL.SP.1992.068.01.02. Bibcode: 1992GSLSP..68...17C. 
  3. ↑ 3.0 3.1 3.2 Bryan, Scott; Ernst, Richard (2007). "Proposed Revision to Large Igneous Province Classification". Earth-Science Reviews 86 (1): 175–202. doi:10.1016/j.earscirev.2007.08.008. Bibcode: 2008ESRv...86..175B. http://www.mantleplumes.org/LIPClass2.html. Retrieved 10 September 2009. 
  4. ↑ 4.0 4.1 Sheth, Hetu C. (2007). "'Large Igneous Provinces (LIPs)': Definition, recommended terminology, and a hierarchical classification". Earth-Science Reviews 85 (3–4): 117–124. doi:10.1016/j.earscirev.2007.07.005. Bibcode: 2007ESRv...85..117S. http://www.mantleplumes.org/WebDocuments/sheth2007-esr.pdf. 
  5. ↑ Svensen, H. H.; Torsvik, T. H.; Callegaro, S.; Augland, L.; Heimdal, T. H.; Jerram, D. A.; Planke, S.; Pereira, E. (2017-08-30). "Gondwana Large Igneous Provinces: plate reconstructions, volcanic basins and sill volumes". Geological Society, London, Special Publications 463 (1): 17–40. doi:10.1144/sp463.7. ISSN 0305-8719. 
  6. ↑ Michael R. Rampino; Richard B. Stothers (1988). "Flood Basalt Volcanism During the Past 250 Million Years". Science 241 (4866): 663–668. doi:10.1126/science.241.4866.663. PMID 17839077. Bibcode: 1988Sci...241..663R. http://pubs.giss.nasa.gov/docs/1988/1988_Rampino_Stothers_1.pdf. [|permanent dead link|dead link}}]
  7. ↑ Eremin, N. I. (2010). "Platform magmatism: Geology and minerageny". Geology of Ore Deposits 52 (1): 77–80. doi:10.1134/S1075701510010071. Bibcode: 2010GeoOD..52...77E. 
  8. ↑ Zhou, Mei-Fu (2008). "Two magma series and associated ore deposit types in the Permian Emeishan large igneous province, SW China". Lithos 103 (3–4): 352–368. doi:10.1016/j.lithos.2007.10.006. Bibcode: 2008Litho.103..352Z. 
  9. ↑ 9.0 9.1 Braun, Jean (2010). "The many surface expressions of mantle dynamics". Nature Geoscience 3 (12): 825–833. doi:10.1038/ngeo1020. Bibcode: 2010NatGe...3..825B. 
  10. ↑ 10.0 10.1 Allen, Philip A (2011). "Geodynamics: Surface impact of mantle processes". Nature Geoscience 4 (8): 498–499. doi:10.1038/ngeo1216. Bibcode: 2011NatGe...4..498A. 
  11. ↑ 11.0 11.1 Humphreys, Eugene; Schmandt, Brandon (2011). "Looking for mantle plumes". Physics Today 64 (8): 34. doi:10.1063/PT.3.1217. Bibcode: 2011PhT....64h..34H. 
  12. ↑ Courtillot, Vincent; Davaille, Anne; Besse, Jean; Stock, Joann (January 2003). "Three distinct types of hotspots in the Earth's mantle". Earth and Planetary Science Letters 205 (3–4): 295–308. doi:10.1016/S0012-821X(02)01048-8. Bibcode: 2003E&PSL.205..295C. 
  13. ↑ E. Humphreys and B. Schmandt; Looking for Mantle Plumes; Physics Today; August 2011; pp. 34–39
  14. ↑ 14.0 14.1 14.2 Hagstrum, Jonathan T. (2005). "Antipodal hotspots and bipolar catastrophes: Were oceanic large-body impacts the cause?". Earth and Planetary Science Letters 236 (1–2): 13–27. doi:10.1016/j.epsl.2005.02.020. Bibcode: 2005E&PSL.236...13H. 
  15. ↑ Jackson, Matthew G.; Carlson, Richard W. (2011). "An ancient recipe for flood-basalt genesis;". Nature 476 (7360): 316–319. doi:10.1038/nature10326. PMID 21796117. Bibcode: 2011Natur.476..316J. 
  16. ↑ Coffin, M.F., Eldholm, O. (Eds.), 1991. Large Igneous Provinces: JOI/USSAC workshop report. The University of Texas at Austin Institute for Geophysics Technical Report, p. 114.
  17. ↑ Coffin, M.F., Eldholm, O., 1992. Volcanism and continental break-up: a global compilation of large igneous provinces. In: Storey, B.C., Alabaster, T., Pankhurst, R.J. (Eds.), Magmatism and the Causes of Continental Break-up. Geological Society of London Special Publication, vol. 68, pp. 17–30.
  18. ↑ Coffin, M.F., Eldholm, O., 1994. Large igneous provinces: crustal structure, dimensions, and external consequences. Reviews of Geophysics Vol. 32, pp. 1–36.
  19. ↑ 19.0 19.1 19.2 19.3 S.E. Bryan & R.E. Ernst; Revised definition of Large Igneous Provinces (LIPs); Earth-Science Reviews Vol. 86 (2008) pp. 175–202
  20. ↑ Ernst, R. E.; Buchan, K. L. (1997), "Giant Radiating Dyke Swarms: Their Use in Identifying Pre-Mesozoic Large Igneous Provinces and Mantle Plumes", Large Igneous Provinces: Continental, Oceanic and Flood Volcanism (Geophysical Monograph 100), Washington D.C.: American Geophysical Union, pp. 297, ISBN 978-0-87590-082-7 
  21. ↑ 21.0 21.1 21.2 21.3 21.4 21.5 21.6 21.7 M.A. Richards, R.A. Duncan, V.E. Courtillot; Flood Basalts and Hot-Spot Tracks: Plume Heads and Tails; SCIENCE, VOL. 246 (1989) 103–108
  22. ↑ 22.0 22.1 Antretter, M.; Riisager, P.; Hall, S.; Zhao, X.; Steinberger, B. (2004). "Modelled palaeolatitudes for the Louisville hot spot and the Ontong Java Plateau". Geological Society, London, Special Publications 229 (1): 21–30. doi:10.1144/GSL.SP.2004.229.01.03. Bibcode: 2004GSLSP.229...21A. http://sp.lyellcollection.org/cgi/content/abstract/229/1/21. 
  23. ↑ 23.0 23.1 Nash, Barbara P.; Perkins, Michael E.; Christensen, John N.; Lee, Der-Chuen; Halliday, A.N. (2006). "The Yellowstone hotspot in space and time: Nd and Hf isotopes in silicic magmas". Earth and Planetary Science Letters 247 (1–2): 143–156. doi:10.1016/j.epsl.2006.04.030. Bibcode: 2006E&PSL.247..143N. 
  24. ↑ 24.0 24.1 24.2 Weis, D. (1993). "The Influence of Mantle Plumes in Generation of Indian Oceanic Crust". Synthesis of Results from Scientific Drilling in the Indian Ocean. Geophysical Monograph Series. 70. 57–89. doi:10.1029/gm070p0057. ISBN 9781118668030. Bibcode: 1992GMS....70...57W. 
  25. ↑ 25.0 25.1 E.V. Verzhbitsky. "Geothermal regime and genesis of the Ninety-East and Chagos-Laccadive ridges." Journal of Geodynamics, Volume 35, Issue 3, April 2003, Pages 289–302
  26. ↑ Sur l'âge des trapps basaltiques (On the ages of flood basalt events); Vincent E. Courtillot & Paul R. Renne; Comptes Rendus Geoscience; Vol: 335 Issue: 1, January 2003; pp: 113–140
  27. ↑ Hoernle, Kaj; Hauff, Folkmar; van den Bogaard, Paul (2004). "70 m.y. history (139–69 Ma) for the Caribbean large igneous province". Geology 32 (8): 697–700. doi:10.1130/g20574.1. Bibcode: 2004Geo....32..697H. http://geology.geoscienceworld.org/cgi/content/abstract/32/8/697. 
  28. ↑ Ernst, Richard E.; Buchan, Kenneth L. (2001). Mantle plumes: their identification through time. Geological Society of America. pp. 143, 145, 146, 147, 148, 259. ISBN 978-0-8137-2352-5. 
  29. ↑ Kerr, AC (December 2005). "Oceanic LIPS: Kiss of death". Elements 1 (5): 289–292. doi:10.2113/gselements.1.5.289. 
  30. ↑ Gohl, K.; Uenzelmann-Neben, G.; Grobys, N. (2011). "Growth and dispersal of a southeast African Large Igenous Province". South African Journal of Geology 114 (3–4): 379–386. doi:10.2113/gssajg.114.3-4.379. Bibcode: 2011SAJG..114..379G. http://epic.awi.de/23393/1/Gohl-etal_Mozambique-Ridge_SAJG_2011.pdf. Retrieved 12 July 2015. 
  31. ↑ 31.0 31.1 31.2 31.3 31.4 31.5 31.6 31.7 31.8 Ross, P.S.; Peateb, I. Ukstins; McClintocka, M.K.; Xuc, Y.G.; Skillingd, I.P.; Whitea, J.D.L.; Houghtone, B.F. (2005). "Mafic volcaniclastic deposits in flood basalt provinces: A review". Journal of Volcanology and Geothermal Research 145 (3–4): 281–314. doi:10.1016/j.jvolgeores.2005.02.003. Bibcode: 2005JVGR..145..281R. http://espace.inrs.ca/1903/1/Ross-et-al%28LIPs%292005-web%5B1%5D.pdf. 
  32. ↑ TH Torsvik, RD Tucker, LD Ashwal, EA Eide, NA Rakotosolofo, MJ de Wit. "Late Cretaceous magmatism in Madagascar: palaeomagnetic evidence for a stationary Marion hotspot." Earth and Planetary Science Letters, Volume 164, Issues 1–2, 15 December 1998, Pages 221–232
  33. ↑ Tegner C.; Storey M.; Holm P.M.; Thorarinsson S.B.; Zhao X.; Lo C.-H.; Knudsen M.F. (March 2011). "Magmatism and Eurekan deformation in the High Arctic Large Igneous Province: 40Ar–39Ar age of Kap Washington Group volcanics, North Greenland". Earth and Planetary Science Letters 303 (3–4): 203–214. doi:10.1016/j.epsl.2010.12.047. Bibcode: 2011E&PSL.303..203T. http://ntur.lib.ntu.edu.tw/bitstream/246246/240518/-1/116.pdf. 
  34. ↑ Knight, K.B.; Nomade S.; Renne P.R.; Marzoli A.; Bertrand H.; Youbi N. (2004). "The Central Atlantic Magmatic Province at the Triassic–Jurassic boundary: paleomagnetic and 40Ar/39Ar evidence from Morocco for brief, episodic volcanism". Earth and Planetary Science Letters 228 (1–2): 143–160. doi:10.1016/j.epsl.2004.09.022. Bibcode: 2004E&PSL.228..143K. 
  35. ↑ Blackburn, Terrence J.; Olsen, Paul E.; Bowring, Samuel A.; McLean, Noah M.; Kent, Dennis V.; Puffer, John; McHone, Greg; Rasbury, Troy et al. (2013). "Zircon U–Pb Geochronology Links the End-Triassic Extinction with the Central Atlantic Magmatic Province". Science 340 (6135): 941–945. doi:10.1126/science.1234204. PMID 23519213. Bibcode: 2013Sci...340..941B. 
  36. ↑ Wingate, MTD; Pirajno, F; Morris, PA (2004). "Warakurna large igneous province: A new Mesoproterozoic large igneous province in west-central Australia". Geology 32 (2): 105–108. doi:10.1130/G20171.1. Bibcode: 2004Geo....32..105W. 
  37. ↑ 37.0 37.1 Sheth, H.C. (2007). "LIP classification". www.mantleplumes.org. http://www.mantleplumes.org/LIPClass.html. 
  38. ↑ Agangi, Andrea (2011). Magmatic and volcanic evolution of a silicic large igneous province (SLIP): the Gawler Range Volcanics and Hiltaba Suite, South Australia (PhD). University of Tasmania. Retrieved 9 January 2022. PDF
  39. ↑ Puchkov, Victor; Ernst, Richard E.; Hamilton, Michael A.; Söderlund, Ulf; Sergeeva, Nina (2016). "A Devonian >2000-km-long dolerite dyke swarm-belt and associated basalts along the Urals-Novozemelian fold-belt: part of an East-European (Baltica) LIP tracing the Tuzo Superswell". GFF 138 (1): 6–16. doi:10.1080/11035897.2015.1118406. Bibcode: 2016GFF...138....6P. 

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