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Caribbean large igneous province

Summary

The Caribbean large igneous province (CLIP) consists of a major flood basalt, which created this large igneous province (LIP). It is the source of the current large eastern Pacific oceanic plateau, of which the Caribbean-Colombian oceanic plateau is the tectonized remnant. The deeper levels of the plateau have been exposed on its margins at the North and South American plates. The volcanism took place between 139 and 69 million years ago, with the majority of activity appearing to lie between 95 and 88 Ma. The plateau volume has been estimated as on the order of 4 x 106 km3. It has been linked to the Galápagos hotspot.[1]

Actual and reconstructed position of the Caribbean plateau

Proto-Caribbean Seaway edit

Divergence between the North American and South American Plates began to create oceanic crust off Colombia's Pacific coast by the end of the Jurassic (150 Ma). This divergence, which continued until at least 66 Ma, first resulted in a "proto-Caribbean spreading ridge" between these plates flanked by a perpendicular transform zone on its Pacific side. By 135–130 Ma, the subduction of the Farallon Plate had begun along this transform zone, effectively modifying it into a subduction zone and beginning the creation of the Great Caribbean Arch. This arch was formed around 120-115 Ma but must have been intersected by the Caribbean spreading ridge until 66 Ma. Hence, the Farallon Plate fed the spreading zone and later became the Caribbean Plate.[2]

LIP formation edit

CLIP formed as a large igneous province and now forms a thickened zone of oceanic crust between the North American and South American Plates.[3] In some places the oceanic crust is 2–3 times as thick as normal oceanic crust (15–20 km (9.3–12.4 mi) vs 7 km (4.3 mi). Its composition is similar to that of the Ontong Java Plateau.[4]

Geochemical and geochronological evidences clearly indicate that the Galápagos hotspot initiated the formation of the CLIP 95-90 Ma in the eastern Pacific. From there it move north-east with the Farallon Plate between the two American plates until it collided with a volcanic arc, the Greater Antilles 60 million years later. Fragments of this voyage is preserved in accreted seamounts along the Central American coast and the Cocos and Carnegie Ridges. Isotopic profiles of Galápagos rocks can be matched with those from CLIP rocks.[3]

92–63 Ma 40Ar/39Ar ages have been reported for the Curaçao Lava Formation and 94–83 ma for the Dumisseau Formation in Haiti, dating both locations back to the original LIP formation 94 Ma. CLIP volcanism originates from the plume-like source distinct from a MORB (mid-ocean ridge basalt) mantle. The long duration of CLIP volcanism can be explained by the interaction between a plume and the Greater Antilles subduction zone.[5]

The margins of the CLIP have been uplifted and are exposed above sea level, which makes it unique among oceanic plateaus. It stretches 2,500 km (1,600 mi) east to west and 1,300 km (810 mi) north to south.[6][7] The CLIP is composed of irregularly thickened (up to 20 km (12 mi)) oceanic crust of the Caribbean Plate and the deformed associated magmatic terranes obducted onto the Pacific coasts of northern South America, Central America, and the Antilles. One of the least deformed parts is Gorgona Island off Colombia's Pacific coast.[6][7][8]

The CLIP was created during three phases of eruptions dating between the Aptian and the Maastrichtian: a first phase 124–112 Ma; the main magma production phase 94–83 Ma; and an 80–72 Ma phase. The youngest igneous rocks, in the Dominican Republic and Costa Rica, are from 63 Ma. That the CLIP originated in the Pacific is obvious because fragments of oceanic crust accreted to the margins of the Caribbean, for example on Hispaniola and Puerto Rico, contain fauna of Pacific provenance.[9]

The Farallon Plate's eastward movement forced the northern half of the CLIP into the ocean basin that had opened between North and South America starting in the Jurassic. However, the mechanisms causing the NE movement of the CLIP remains unclear, especially considering the subduction in the Costa Rica-Panama arc initiated during the Campanian (83–72 Ma). The Galápagos hotspot is probably responsible for the main plume-related magmatic event 90 Ma, whilst the 76 Ma and 55 Ma event are related to lithospheric thinning in the Central Caribbean.[9]

40Ar/39Ar dating have determined that the main magmatism occurred 95 to 83 million years ago (Ma) while a second pulse occurred 81-69 Ma. Around 86 Ma the arrival of a large plume initiated the Galápagos hotspot which resulted in volcanism over large parts of the Caribbean Plate and north-west South America. Renewed volcanism about 75 Ma has been attributed to either the Galápagos hotspot, thinning of the lithosphere coupled with associated melting and upwelling of plume-head material, or both.[6]

Seismic and geochemical analyses, on the other hand, suggest the CLIP consists of several oceanic plateaus and palaeo-hotspot tracks formed 139-83 Ma some of which have been overprinted by later magmatism.[6][10] If these first volcanic activities were generated by the Galápagos hotspot, it would make it the oldest still active hotspot on Earth.[10]

See also edit

References edit

Notes edit

  1. ^ Courtillot & Renne 2003; Hoernle, Hauff & van den Bogaard 2004
  2. ^ Serrano et al. 2011, 5.2. Geodynamic setting during the formation of the CLIP, p. 332; Fig. 8, p. 333
  3. ^ a b Loewen et al. 2013, Introduction, pp. 4241–4242
  4. ^ Hauff et al. 2000, 2. Geological background, pp. 248–249
  5. ^ Loewen et al. 2013, Conclusions, pp. 4256–4257
  6. ^ a b c d Courtillot & Renne 2003, Introduction, p. 697
  7. ^ a b Geldmacher et al. 2003, Introduction
  8. ^ Serrano et al. 2011, Introduction, pp. 324–325
  9. ^ a b Escuder-Viruete et al. 2011, The Caribbean large igneous province, p. 309
  10. ^ a b Courtillot & Renne 2003, p. 700

Sources edit

  • Courtillot, V. E.; Renne, P. R. (2003). "On the ages of flood basalt events (Sur l'âge des trapps basaltiques)" (PDF). Comptes Rendus Geoscience. 335 (1): 113–140. Bibcode:2003CRGeo.335..113C. CiteSeerX 10.1.1.461.3338. doi:10.1016/S1631-0713(03)00006-3. Retrieved 9 August 2015.
  • Escuder-Viruete, J.; Pérez-Estaun, A.; Joubert, M.; Weis, D. (2011). "The Pelona-Pico Duarte basalts Formation, Central Hispaniola: an on-land section of Late Cretaceous volcanism related to the Caribbean large igneous province" (PDF). Geologica Acta. 9 (3–4): 307–328. doi:10.1344/105.000001716. Retrieved 9 August 2015.
  • Geldmacher, J.; Hanan, B. B.; Blichert‐Toft, J.; Harpp, K.; Hoernle, K.; Hauff, F.; Werner, R.; Kerr, A. C. (2003). "Hafnium isotopic variations in volcanic rocks from the Caribbean Large Igneous Province and Galápagos hot spot tracks" (PDF). Geochemistry, Geophysics, Geosystems. 4 (7): 1062. Bibcode:2003GGG.....4.1062G. doi:10.1029/2002GC000477. S2CID 13509777.
  • Hauff, F.; Hoernle, K.; Tilton, G.; Graham, D. W.; Kerr, A. C. (2000). "Large volume recycling of oceanic lithosphere over short time scales: geochemical constraints from the Caribbean Large Igneous Province" (PDF). Earth and Planetary Science Letters. 174 (3): 247–263. Bibcode:2000E&PSL.174..247H. doi:10.1016/s0012-821x(99)00272-1. Retrieved 16 August 2015.
  • Hoernle, K.; Hauff, F.; van den Bogaard, P. (2004). "70 m.y. history (139–69 Ma) for the Caribbean large igneous province". Geology. 32 (8): 697–700. Bibcode:2004Geo....32..697H. doi:10.1130/G20574.1. Retrieved 9 August 2015.
  • Loewen, M. W.; Duncan, R. A.; Kent, A. J. R.; Krawl, K. (2013). "Prolonged plume volcanism in the Caribbean Large Igneous Province: New insights from Curaçao and Haiti" (PDF). Geochemistry, Geophysics, Geosystems. 14 (10): 4241–4259. Bibcode:2013GGG....14.4241L. doi:10.1002/ggge.20273. S2CID 56052663. Retrieved 9 August 2015.
  • Serrano, L.; Ferrari, L.; Martínez, M. L.; Petrone, C. M.; Jaramillo, C. (2011). "An integrative geologic, geochronologic and geochemical study of Gorgona Island, Colombia: Implications for the formation of the Caribbean Large Igneous Province" (PDF). Earth and Planetary Science Letters. 309 (3): 324–336. Bibcode:2011E&PSL.309..324S. doi:10.1016/j.epsl.2011.07.011. Retrieved 9 August 2015.

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