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Huge regional accumulation of igneous rocks From Wikipedia, the free encyclopedia
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.
In 1992, Coffin and Eldholm initially defined the term "large igneous province" 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."[2][3][4] That original definition included continental flood basalts, oceanic plateaus, large dike swarms (the eroded roots of a volcanic province), and volcanic rifted margins. Mafic basalt sea floors and other geological products of 'normal' plate tectonics were not included in the definition.[5] 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. 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—parts of which are found in Brazil, eastern North America, and northwestern Africa.[6]
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.[7]
The definition has since been expanded and refined, and remains a work in progress. Some new definitions of 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. 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.[8] LIP is now frequently used to also describe voluminous areas of, not just mafic, but all types of igneous rocks. Further, the minimum threshold to be included as a LIP has been lowered to 50,000 km2.[8] The working taxonomy, focused heavily on geochemistry, is:
Because large igneous provinces are created during short-lived igneous events resulting in relatively rapid and high-volume accumulations of volcanic and intrusive igneous rock, they warrant study. LIPs present possible links to mass extinctions and global environmental and climatic changes. Michael Rampino and Richard Stothers cite 11 distinct flood basalt episodes—occurring in the past 250 million years—which created volcanic provinces and oceanic plateaus and coincided with mass extinctions.[9] 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.[10] They are also associated with formation of major mineral provinces including platinum group element deposits and, in the silicic LIPs, silver and gold deposits.[5] Titanium and vanadium deposits are also found in association with LIPs.[11]
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.[5] Some of these changes were related to rapid release of greenhouse gases from the lithosphere 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.[12] LIPs have played a major role in the cycles of continental breakup, continental formation, new crustal additions from the upper mantle, and supercontinent cycles.[12]
Earth has an outer shell made 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 mantle plumes of hot material from lower levels. The surface of the Earth reflects stretching, thickening and bending of the tectonic plates as they interact.[13]
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.[14]
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.[13] These ascending plumes play an important role in LIP formation.
When created, LIPs often have an areal extent of a few million square kilometers and volumes on the order of 1 million cubic kilometers. 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. The source of many or all LIPs are variously attributed to mantle plumes, to processes associated with plate tectonics or to meteorite impacts.
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.[14]
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.[15]
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 convoluted vertical paths with varying quantities of hotter material, even at depths where crystallographic transformations are predicted to occur.[16][clarification needed]
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.[17]
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.[18]
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.[17]
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 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.[17]
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.[7]
Giant dyke swarms having lengths over 300 km[19] 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.[7]
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.[7]
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:
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 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, indicative of lower temperature, dense media.
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.[20][21]
| Province | Region | Hotspot | Reference |
|---|---|---|---|
| Columbia River Basalt | Northwestern US | Yellowstone hotspot | [20][22] |
| Ethiopia-Yemen Flood Basalts | Ethiopia, Yemen | [20] | |
| North Atlantic Igneous Province | Northern Canada, Greenland, the Faeroe Islands, Norway, Ireland and Scotland | Iceland hotspot | [20] |
| Deccan Traps | India | Réunion hotspot | [20] |
| Rajmahal Traps | Eastern India | Ninety East Ridge | [23][24] |
| Kerguelen Plateau | Indian Ocean | Kerguelen hotspot | [23] |
| Ontong Java Plateau | Pacific Ocean | Louisville hotspot | [20][21] |
| Paraná and Etendeka traps | Brazil–Namibia | Tristan hotspot | [20] |
| Karoo-Ferrar Province | South Africa, Antarctica, Australia & New Zealand | Marion Island | [20] |
| Caribbean large igneous province | Caribbean-Colombian oceanic plateau | Galápagos hotspot | [25][26] |
| Mackenzie Large Igneous Province | Canadian Shield | Mackenzie hotspot | [27] |
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.[28]
Large igneous provinces are associated with a handful of ore deposit types including:
Enrichment in mercury relative to total organic carbon (Hg/TOC) is a common geochemical proxy used to detect massive volcanism in the geologic record, although its foolproofness has been called into question.[29]
| 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 | [22][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 | [31] | |
| Deccan Traps | India | 66 | 0.5–0.8 | 0.5–1.0 | [31] | |
| Madagascar | 88 | [32] | ||||
| Rajmahal Traps | India | 116 | [23][24] | |||
| 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 | [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] |
These LIPs are composed dominantly of felsic materials. Examples include:
These LIPs are comprised dominantly of andesitic materials. Examples include:
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.
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