From Wikipedia, the free encyclopedia
Map of Pangaea with Laurasia and Gondwana. 200 mya
Historical continent
Formed 600 Mya
Type Supercontinent
Today part of Africa
North America
South America
Smaller continents Atlantica
Tectonic plate African Plate
Antarctic Plate
Indo-Australian Plate
South American Plate

Gondwana ( /ɡɒndˈwɑːnə/),[1] or Gondwanaland,[2] was a supercontinent that formed from the unification of several cratons in the Late Neoproterozoic, merged with Laurussia in the Carboniferous to form Pangaea, and began to fragment in the Mesozoic. It was the largest continental landmass on Earth, covering an area of 100,000,000 km2 (39,000,000 sq mi) or 64% of today's continents.[3] Located in the Southern Hemisphere, it incorporated several modern landmasses, including Antarctica, South America, Africa, Madagascar, and Australia, as well as the Arabian Peninsula and the Indian subcontinent, which have now moved entirely into the Northern Hemisphere.

The formation of Gondwana began c. 800 to 650 Ma with the East African orogeny — the collision of India, Madagascar, and Sri Lanka with East Africa — and was completed c. 600 to 530 Ma with the overlapping Brasiliano and Kuunga orogenies — the collision of South America with Africa and the addition of Australia and Antarctica, respectively.[4]

Origin of concept

The continent of Gondwana was named by Austrian scientist Eduard Suess, after the Gondwana region of central northern India which is derived from Sanskrit for "forest of the Gonds". The name had been previously used in a geological context, first by H.B. Medlicott in 1872,[5] from which the Gondwana sedimentary sequences (Permian-Triassic) are also described. The term "Gondwanaland" is preferred by some scientists in order to make a clear distinction between the region and the supercontinent.[6]


Eastern Gondwana. 620 to 550 Ma post-collisional extension of the East African Orogeny in blue and 570 to 530 Ma collisional metamorphism of the Kuunga orogeny in red.[7]

The assembly of Gondwana was a protracted process that occurred during the Neoproterozoic and Paleozoic which remains relatively poorly constrained because of the lack of paleo-magnetic data. Several orogenies, collectively known as the Pan-African orogeny, led to the amalgamation of most of the continental fragments of a much older supercontinent, Rodinia. One of those orogenic belts, the Mozambique Belt, formed c. 800 to 650 Ma and was originally interpreted as the suture between East (India, Madagascar, Antarctica, and Australia) and West Gondwana (Africa and South America). Three orogenies were recognized during the 1990s: the East African orogeny (650 to 800 Ma) and Kuunga orogeny (including the Malagasy orogeny in southern Madagascar) (550 Ma) — the collision between East Gondwana and East Africa in two steps, and the Brasiliano orogeny (660 to 530 Ma) — the collision between South American and African cratons.[8]

The final stages of Gondwanan assembly overlapped with the opening of the Iapetus Ocean between Laurentia and western Gondwana.[9] During this interval, the Cambrian explosion occurred. Laurentia was docked against the western shores of a united Gondwana for a short period near the Precambrian/Cambrian boundary, forming the short-lived and still disputed supercontinent Pannotia.[10]

The Mozambique Ocean separated the CongoTanzaniaBangweulu Block of central Africa from Neoproterozoic India (India, the Antongil Block in far eastern Madagascar, the Seychelles, and the Napier and Rayner Complexes in East Antarctica). The Azania continent[11] (much of central Madagascar, the Horn of Africa and parts of Yemen and Arabia) was an island in the Mozambique Ocean.

The Australia/Mawson continent was still separated from India, eastern Africa, and Kalahari by c. 600 Ma when most of western Gondwana had already been amalgamated. By c. 550 Ma, India had reached its Gondwana position which initiated the Kuunga orogeny (also known as the Pinjarra orogeny). Meanwhile, on the other side of the forming Africa, Kalahari collided with Congo and Rio de la Plata which closed the Adamastor Ocean. c. 540–530 Ma the closure of the Mozambique Ocean brought India next to Australia–East Antarctica and both North and South China were located in proximity to Australia.[12]

Other blocks which helped to form parts of the Southern Cone of South America, including a piece transferred from Laurentia when the west edge of Gondwana scraped against southeast Laurentia in the Ordovician.[13] This is the Cuyania or Precordillera terrane of the Famatinian orogeny in northwest Argentina which may have continued the line of the Appalachians southwards,[14]

Reconstruction showing final stages of assembly of Gondwana, 550 Mya

As the rest of Gondwana formed, a complex series of orogenic events assembled the eastern parts of Gondwana (eastern Africa, Arabian-Nubian Shield, Seychelles, Madagascar, India, Sri Lanka, East Antarctica, and Australia) c. 750 to 530 Ma. First the Arabian-Nubian Shield collided with eastern Africa (in the Kenya-Tanzania region) in the East African Orogeny c.750 to 620 Ma. Then Australia and East Antarctica were merged with the remaining Gondwana c. 570 to 530 Ma in the Kuunga Orogeny.[15]

The later Malagasy orogeny at about 550–515 Mya affected Madagascar, eastern East Africa and southern India. In it, Neoproterozoic India collided with the already combined Azania and Congo–Tanzania–Bangweulu Block, suturing along the Mozambique Belt.[16]

The 18,000 km (11,000 mi)-long Terra Australis Orogen developed along Gondwana's western, southern, and eastern margins.[17] Proto-Gondwanan Cambrian arc belts from this margin have been found in eastern Australia, Tasmania, New Zealand, and Antarctica. Though these belts formed a continuous arc chain, the direction of subduction was different between the Australian-Tasmanian and New Zealand-Antarctica arc segments.[18]


Gondwana and Laurussia formed the Pangaea supercontinent during the Carboniferous. Pangaea began to break up in the Mid-Jurassic when the Central Atlantic opened.[19]

In the western end of Pangaea, the collision between Gondwana and Laurussia closed the Rheic and Palaeo-Tethys oceans. The obliquity of this closure resulted in the docking of some northern terranes in the Marathon, Ouachita, Alleghanian, and Variscan orogenies, respectively. Southern terranes, such as Chortis and Oaxaca, on the other hand, remained largely unaffected by the collision along the southern shores of Laurentia. Some Peri-Gondwanan terranes, such as Yucatán and Florida, were buffered from collisions by major promontories. Other terranes, such as Carolina and Meguma, were directly involved in the collision. The final collision resulted in the Variscan-Appalachian Mountains, stretching from present-day Mexico to southern Europe. Meanwhile, Baltica collided with Siberia and Kazakhstania which resulted in the Uralian orogeny and Laurasia. Pangaea was finally amalgamated in the Late Carboniferous-Early Permian but the oblique forces continued until Pangaea began to rift in the Triassic.[20]

In the eastern end collisions occurred slightly later. The North China, South China, and Indochina blocks rifted from Gondwana during the middle Paleozoic and opened the Proto-Tethys Ocean. North China docked with Mongolia and Siberia during the Carboniferous–Permian followed by South China. The Cimmerian blocks then rifted from Gondwana to form the Palaeo-Thethys and Neo-Tethys oceans in the Late Carboniferous and docked with Asia during the Triassic and Jurassic. Western Pangaea began to rift while the eastern end was still being assembled.[21]

The formation of Pangaea and its mountains had a tremendous impact on global climate and sea levels, which resulted in glaciations and continent-wide sedimentation. In North America, the base of the Absaroka sequence coincides with the Alleghanian and Ouachita orogenies and are indicative of a large-scale change in the mode of deposition far away from the Pangaean orogenies. Ultimately, these changes contributed to the Permian–Triassic extinction event and left large deposits of hydrocarbons, coal, evaporite, and metals.[22]

The break-up of Pangaea began with the Central Atlantic magmatic province (CAMP) between South America, Africa, North America, and Europe. CAMP covered more than seven million square kilometres over a few million years, reached its peak at c. 200 Ma, and coincided with the Triassic–Jurassic extinction event.[23] The reformed Gondwanan continent was not precisely the same as that which had existed before Pangaea formed; for example, most of Florida and southern Georgia and Alabama is underlain by rocks that were originally part of Gondwana, but this region stayed attached to North America when the Central Atlantic opened.[24]


A large number of terranes were accreted to Eurasia during Gondwana's existence but the Cambrian or Precambrian origin of many of these terranes remains uncertain. For example, some Palaeozoic terranes and microcontinents that now make up Central Asia, often called the "Kazakh" and "Mongolian terranes", were progressively amalgamated into the continent Kazakhstania in the Late Silurian. Whether these blocks originated on the shores of Gondwana is not known.[25]

In the Early Palaeozoic the Armorican terrane, which today form large parts of France, was part of either Peri-Gondwana or core Gondwana; the Rheic Ocean closed in front of it and the Palaeo-Tethys Ocean opened behind it. Precambrian rocks from the Iberian Peninsula suggest it too probably formed part of core Gondwana before its detachment as an orocline in the Variscan orogeny close to the Carboniferous–Permian boundary.[26]



Antarctica, the centre of the supercontinent, shared boundaries with all other Gondwana continents and the fragmentation of Gondwana propagated clockwise around it. The break-up was the result of one of the Earth's most extensive large igneous provinces c. 200 to 170 Ma, but the oldest magnetic anomalies between South America, Africa, and Antarctica are found in what is now the southern Weddell Sea where initial break-up occurred during the Jurassic c. 160 to 180 Ma.[27]

Opening of western Indian Ocean

Gondwana began to break up in the early Jurassic following the extensive and fast emplacement of the Karoo-Ferrar flood basalts c. 184 Ma. Before the Karoo plume initiated rifting between Africa and Antarctica, it separated a series of smaller continental blocks from Gondwana's southern, Proto-Pacific margin (along what is now the Transantarctic Mountains): the Antarctic Peninsula, Marie Byrd Land, Zealandia, and Thurston Island; the Falkland Islands and Ellsworth–Whitmore Mountains (in Antarctica) were rotated 90° in opposite directions; and South America south of the Gastre Fault (often referred to as Patagonia) was pushed westward.[28] The history of the Africa-Antarctica break-up can be studied in great detail in the fracture zones and magnetic anomalies flanking the Southwest Indian Ridge.[29]

The Madagascar block and the Mascarene Plateau, stretching from the Seychelles to Réunion, were broken off India; elements of this breakup nearly coincide with the Cretaceous–Paleogene extinction event. The India–Madagascar–Seychelles separations appear to coincide with the eruption of the Deccan basalts, whose eruption site may survive as the Réunion hotspot. The Seychelles and the Maldives are now separated by the Central Indian Ridge.

Opening of eastern Indian Ocean

East Gondwana, comprising Antarctica, Madagascar, India, and Australia, began to separate from Africa. East Gondwana then began to break up c. 132.5 to 96 Ma when India moved northwest from Australia-Antarctica.[30] The Indian Plate and the Australian Plate are now separated by the Capricorn Plate and its diffuse boundaries.[31] During the opening of the Indian Ocean, the Kerguelen hotspot first formed the Kerguelen Plateau on the Antarctic Plate c. 118 to 95 Ma and then the Ninety East Ridge on the Indian Plate at c. 100 Ma.[32] The Kerguelen Plateau and the Broken Ridge, the southern end of the Ninety East Ridge, are now separated by the Southeast Indian Ridge.

Separation between Australia and East Antarctica began c. 132 Ma with sea-floor spreading occurring c. 96 Ma. A shallow seaway developed over the South Tasman Rise during the Early Cenozoic and as oceanic crust started to separate the continents during the Eocene c. 35.5 Ma global ocean temperature dropped significantly.[33] A dramatic shift from arc- to rift magmatism c. 100 Ma separated Zealandia, including New Zealand, the Campbell Plateau, Chatham Rise, Lord Howe Rise, Norfolk Ridge, and New Caledonia, from West Antarctica c. 84 Ma.[34]

Opening of South Atlantic Ocean

The opening of the South Atlantic Ocean divided West Gondwana (South America and Africa), but there considerable debate over the exact timing of this break-up. Rifting propagated from south to north along Triassic–Early Jurassic lineaments, but intra-continental rifts also began to develop within both continents in Jurassic–Cretaceous sedimentary basins; subdividing each continent into three sub-plates. Rifting began c. 190 Ma at Falkland latitudes, forcing Patagonia to move relative to the still static remainder of South America and Africa, and this westward movement lasted until the Early Cretaceous 126.7 Ma. From there rifting propagated northward during the Late Jurassic c. 150 Ma or Early Cretaceous c. 140 Ma most likely forcing dextral movements between sub-plates on either side. South of the Walvis Ridge and Rio Grande Rise the Paraná and Etendeka magmatics resulted in further ocean-floor spreading c. 130 to 135 Ma and the development of rifts systems on both continents, including the Central African Rift System and the Central African Shear Zone which lasted until c. 85 Ma. At Brazilian latitudes spreading is more difficult to assess because of the lack of palaeo-magnetic data, but rifting occurred in Nigeria at the Benue Trough c. 118 Ma. North of the Equator the rifting began after 120.4 Ma and continued until c. 100 to 96 Ma.[35]


As the age of mammals commenced, the continent of Australia-New Guinea began gradually to separate and move north (55 Mya), rotating about its axis to begin with, and thus retaining some connection with the remainder of Gondwana for about 10 million years.

About 45 Mya, the Indian subcontinent collided with Asia, buckling the crust and forming the Himalayas. At about the same time, the southernmost part of Australia (modern Tasmania) finally separated from Antarctica, letting ocean currents flow between the two continents for the first time. Antarctica became cooler and Australia became drier because ocean currents circling Antarctica were no longer directed around northern Australia into the subtropics.

The opening of the Drake Passage, the separation of South America from West Antarctica, during the Oligocene at c. 30 Ma also caused climate changes.[36] Immediately before this separation, South America and East Antarctica were not connected directly. However, the many microplates of the Antarctic Peninsula remained near southern South America, acting as "stepping stones" and allowing continued biological interchange and stopped oceanic current circulation. When the Drake Passage opened, a barrier was no longer present to force the cold waters of the Southern Ocean to be exchanged with warmer tropical water. Instead, a cold circumpolar current developed and Antarctica became what it is today: a frigid continent that locks up much of the world's fresh water as ice. Sea temperatures dropped by almost 10 °C, and the global climate became much colder.

By about 15 Mya, the collision between New Guinea (on the leading edge of the Australian Plate) and the southwestern part of the Pacific Plate pushed up the New Guinea Highlands, causing a rain shadow effect which drastically changed weather patterns in Australia, drying it out.

Later, South America was connected to North America via the Isthmus of Panama, cutting off a circulation of warm water and thereby making the Arctic colder,[37] as well as allowing the Great American Interchange.

The Red Sea and East African Rift are modern examples of continental rifting.


The Nothofagus plant genus illustrates Gondwanan distribution, having descended from the supercontinent and existing in present-day Australia, New Zealand, New Caledonia, and the Southern Cone. Fossils have also recently been found in Antarctica.[38]

The adjective "Gondwanan" is in common use in biogeography when referring to patterns of distribution of living organisms, typically when the organisms are restricted to two or more of the now-discontinuous regions that were once part of Gondwana, including the Antarctic flora.[6] For example, the plant family Proteaceae, known from all continent in the Southern Hemisphere, has a "Gondwanan distribution" and is often described as an archaic, or relict, lineage. The distributions in Proteaceae is, nevertheless, the result of both Gondwanan rafting and later oceanic dispersal.[39]

During the late Paleozoic, Gondwana extended from a point at or near the South Pole to near the Equator. Across much of Gondwana, the climate was mild. During the Mesozoic, the world was on average considerably warmer than it is today. Gondwana was then host to a huge variety of flora and fauna for many millions of years. The laurel forest of Australia, New Caledonia, and New Zealand have a number of other related species of the laurissilva de Valdivia, through the connection of the Antarctic flora as gymnosperms and deciduous angiosperm Nothofagus. Corynocarpus laevigatus is called the bay of New Zealand, Laurelia novae-zelandiae belongs to the same genus Laurelia. The sempervirens tree niaouli grows in Australia, New Caledonia, and New Zealand.

New Caledonia and New Zealand ecoregions became separated from Australia by continental drift 85 million years ago. The islands still retain plants that originated in Gondwana and spread to the Southern Hemisphere continents later. However, strong evidence exists of glaciation during the Carboniferous to Permian time, especially in South Africa.

See also



  1. ^ "Gondwana". Dictionary.com. Lexico Publishing Group. Retrieved 18 January 2010. 
  2. ^ "Gondwanaland". Merriam-Webster Online Dictionary. Retrieved 18 January 2010. 
  3. ^ Torsvik & Cocks 2013, Abstract
  4. ^ Meert & Van Der Voo 1997, Abstract
  5. ^ Suess 1885, p. 768: "Wir nennen es Gondwána-Land, nach der gemeinsamen alten Gondwána-Flora, … " (We name it Gondwána-Land, after the common ancient flora of Gondwána …)
  6. ^ a b McLoughlin 2001, Gondwana or Gondwanaland?, pp. 272–273
  7. ^ Meert 2003, Fig. 10, p. 19
  8. ^ Meert & Van Der Voo 1997, Introduction, pp. 223–226
  9. ^ Miashita & Yamamoto 1996
  10. ^ Meert & Van Der Voo 1997, p. 229
  11. ^ Defined but not named in Collins & Pisarevsky 2005: "Azania" was a Greek name for the East African coast
  12. ^ Li et al. 2008, The birth of Gondwanaland (600–530 Ma), p. 201
  13. ^ Rapalini 2001; Rapalini 1998, pp. 105–106
  14. ^ Dalla Salda et al. 1998, Abstract; Vujovich, van Staal & Davis 2004, Conclusions, p. 1053
  15. ^ Meert 2003, Abstract
  16. ^ Grantham, Maboko & Eglington 2003
  17. ^ Cawood 2005, Definition and Tectonic Framework, pp. 4–6
  18. ^ Münker & Crawford 2000, Abstract
  19. ^ Torsvik & Van Der Voo 2002, Data selection and reconstruction fits, p. 772
  20. ^ Blakey 2003, Assembly of Western Pangaea: Carboniferous–Permian, pp. 453–454
  21. ^ Blakey 2003, Assembly of Eastern Pangaea: Late Permian–Jurassic, p. 454
  22. ^ Blakey 2003, Summary: significance of Pangaean events, pp. 454–455
  23. ^ Marzoli et al. 1999, Abstract
  24. ^ "Gondwana Remnants In Alabama And Georgia: Uchee Is An 'Exotic' Peri-Gondwanan Arc Terrane, Not Part Of Laurentia". ScienceDaily. February 4, 2008. Retrieved 2011-10-22. 
  25. ^ Torsvik & Cocks 2013, Marginal microcontinents and terranes, p. 1008
  26. ^ Torsvik & Cocks 2013, Southern Europe, pp. 1008–1009
  27. ^ Jokat et al. 2003, Introduction, pp. 1–2
  28. ^ Encarnación et al. 1996, Early rifting and Gondwana breakup, pp. 537–538
  29. ^ Royer et al. 1988, Figg. 7 a–j, pp. 248–257
  30. ^ Powell, Roots & Veevers 1988, Abstract
  31. ^ DeMets, Gordon & Royer 2005, Introduction; Fig. 1, p. 446
  32. ^ Müller, Royer & Lawver 1993, Model results, pp. 277–278
  33. ^ McLoughlin 2001, East Antarctica–Australia, p. 280
  34. ^ McLoughlin 2001, West Antarctica–Tasmantia, p. 280
  35. ^ Seton et al. 2012, South Atlantic, pp. 217–218
  36. ^ Dalziel & Elliot 1982, Antarctica in Gondwanaland, pp. 3–5
  37. ^ Luyendyk, Forsyth & Phillips 1972, Abstract
  38. ^ HaoMin & ZheKun 2007
  39. ^ Barker et al. 2007, Abstract


  • Barker, N. P.; Weston, P. H.; Rutschmann, F.; Sauquet, H. (2007). "Molecular dating of the ‘Gondwanan’plant family Proteaceae is only partially congruent with the timing of the break‐up of Gondwana" (PDF). Journal of Biogeography. 34 (12): 2012–2027. doi:10.1111/j.1365-2699.2007.01749.x. Retrieved 3 September 2017. 
  • Blakey, R. C. (2003). "Carboniferous–Permian paleogeography of the assembly of Pangaea". In Wong, Th. E. Proceedings of the XVth International Congress on Carboniferous and Permian Stratigraphy. Utrecht (Vol. 10, p. 16) (PDF). Utrecht, the Netherlands: Royal Netherlands Academy of Arts and Sciences. Retrieved 16 September 2017. 
  • Cawood, Peter A. (2005). "Terra Australis Orogen: Rodinia breakup and development of the Pacific and Iapetus margins of Gondwana during the Neoproterozoic and Paleozoic". Earth-Science Reviews. 69: 249–279. doi:10.1016/j.earscirev.2004.09.001. 
  • Collins, A. S.; Pisarevsky, S. A. (2005). "Amalgamating eastern Gondwana: The evolution of the Circum-Indian Orogens" (PDF). Earth-Science Reviews. 71 (3–4): 229–270. Bibcode:2005ESRv...71..229.. doi:10.1016/j.earscirev.2005.02.004. Retrieved 4 September 2017. 
  • Dalla Salda, L. H.; de Luchi, M. G. L.; Cingolani, C. A.; Varela, R. (1998). "Laurentia-Gondwana collision: the origin of the Famatinian-Appalachian orogenic belt (a review)" (PDF). Geological Society, London, Special Publications. 142 (1): 219–234. doi:10.1144/GSL.SP.1998.142.01.11. Retrieved 10 September 2017. 
  • Dalziel, I. W. D.; Elliot, D. H. (1982). "West Antarctica: Problem Child of Gondwanaland" (PDF). Tectonics. 1 (1): 3–19. ISSN 1944-9194. doi:10.1029/TC001i001p00003. Retrieved 1 September 2017. 
  • DeMets, C.; Gordon, R. G.; Royer, J. Y. (2005). "Motion between the Indian, Capricorn and Somalian plates since 20 Ma: implications for the timing and magnitude of distributed lithospheric deformation in the equatorial Indian ocean" (PDF). Geophysical Journal International. 161 (2): 445–468. doi:10.1111/j.1365-246X.2005.02598.x. Retrieved 1 October 2017. 
  • Encarnación, J.; Fleming, T. H.; Elliot, D. H.; Eales, H. V. (1996). "Synchronous emplacement of Ferrar and Karoo dolerites and the early breakup of Gondwana" (PDF). Geology. 24 (6): 535–538. ISSN 0091-7613. doi:10.1130/0091-7613(1996)0242.3.CO;2. 
  • Grantham, G. H.; Maboko, M.; Eglington, B. M. (2003). "A review of the evolution of the Mozambique Belt and implications for the amalgamation and dispersal of Rodinia and Gondwana" (PDF). Geological Society, London, Special Publications. 206 (1): 401–425. doi:10.1144/GSL.SP.2003.206.01.19. Retrieved 3 September 2017. 
  • HaoMin, Li; ZheKun, Zhou (1 September 2007). "Fossil Nothofagaceous Leaves from the Eocene of Western Antarctica and their Bearing on the Origin, Dispersal and Systematics of Nothofagus" (PDF). Science in China Series D: Earth Sciences. 50 (10): 1525–1535. doi:10.1007/s11430-007-0102-0. Retrieved 10 September 2017. 
  • Jokat, W.; Boebel, T.; König, M.; Meyer, U. (2003). "Timing and geometry of early Gondwana breakup" (PDF). Journal of Geophysical Research: Solid Earth. 108 (B9). doi:10.1029/2002JB001802. Retrieved 1 October 2017. 
  • Li, Z. X.; Bogdanova, S. V.; Collins, A. S.; Davidson, A.; De Waele, B.; Ernst, R. E.; Fitzsimons, I. C. W.; Fuck, R. A.; Gladkochub, D. P.; Jacobs, J.; Karlstrom, K. E.; Lu, S.; Natapov, L. M.; Pease, V.; Pisarevsky, S. A.; Thrane, K.; Vernikovsky, V. (2008). "Assembly, configuration, and break-up history of Rodinia: a synthesis" (PDF). Precambrian research. 160 (1): 179–210. doi:10.1016/j.precamres.2007.04.021. Retrieved 30 September 2017. 
  • Luyendyk, B. P.; Forsyth, D.; Phillips, J. D. (1972). "Experimental Approach to the Paleocirculation of the Oceanic Surface Waters" (PDF). Geological Society of America Bulletin. 83 (9). doi:10.1130/0016-7606(1972)83[2649:eattpo]2.0.co;2. Retrieved 1 September 2017. 
  • Marzoli, A.; Renne, P. R.; Piccirillo, E. M.; Ernesto, M.; Bellieni, G.; De Min, A. (1999). "Extensive 200-million-year-old continental flood basalts of the Central Atlantic Magmatic Province" (PDF). Science. 284 (5414): 616–618. doi:10.1126/science.284.5414.616. Retrieved 1 October 2017. 
  • McLoughlin, S. (2001). "The breakup history of Gondwana and its impact on pre-Cenozoic floristic provincialism" (PDF). Australian Journal of Botany. 49 (3): 271–300. doi:10.1071/BT00023. Retrieved 3 September 2017. 
  • Meert, J. G. (2003). "A synopsis of events related to the assembly of eastern Gondwana" (PDF). Tectonophysics. 362 (1): 1–40. Bibcode:2003Tectp.362....1M. doi:10.1016/S0040-1951(02)00629-7. 
  • Meert, J. G.; Van Der Voo, R. (1997). "The assembly of Gondwana 800-550 Ma" (PDF). Journal of Geodynamics. 23 (3-4): 223–235. doi:10.1016/S0264-3707(96)00046-4. Retrieved 3 September 2017. 
  • Miashita, Y.; Yamamoto, T. (1996). "Gondwanaland: Its Formation, Evolution and Dispersion". Journal of African Earth Sciences. 23 (2). doi:10.1016/s0899-5362(97)86882-0. 
  • Müller, R. D.; Royer, J. Y.; Lawver, L. A. (1993). "Revised plate motions relative to the hotspots from combined Atlantic and Indian Ocean hotspot tracks" (PDF). Geology. 21 (3): 275–278. doi:10.1130/0091-7613(1993)021<0275:RPMRTT>2.3.CO;2. Retrieved 1 September 2017. 
  • Münker, C.; Crawford, A. J. (2000). "Cambrian arc evolution along the SE Gondwana active margin: a synthesis from Tasmania‐New Zealand‐Australia‐Antarctica correlations" (PDF). Tectonics. 19 (3): 415–432. doi:10.1029/2000TC900002. Retrieved 8 October 2017. 
  • Powell, C.; Roots, S. R.; Veevers, J. J. (1988). "Pre-Breakup Continental Extension in East Gondwanaland and the Early Opening of the Eastern Indian Ocean". Tectonophysics. 155 (1-4): 261–283. doi:10.1016/0040-1951(88)90269-7. 
  • Rapalini, A. E. (2001). The Assembly of Southern South America in the Late Proterozoic and Paleozoic: Some Paleomagnetic Clues. Spring Meeting 2001. American Geophysical Union. Bibcode:2001AGUSM..GP32D03R. Retrieved 18 January 2010. 
  • Rapalini, A. E. (1998). "Syntectonic magnetization of the mid-Palaeozoic Sierra Grande Formation: further constraints on the tectonic evolution of Patagonia" (PDF). Journal of the Geological Society. 155 (1): 105–114. doi:10.1144/gsjgs.155.1.0105. Retrieved 10 September 2017. 
  • Royer, J. Y.; Patriat, P.; Bergh, H. W.; Scotese, C. R. (1988). "Evolution of the Southwest Indian Ridge from the Late Cretaceous (anomaly 34) to the Middle Eocene (anomaly 20)" (PDF). Tectonophysics. 155 (1–4): 235–260. doi:10.1016/0040-1951(88)90268-5. Retrieved 31 July 2016. 
  • Seton, M.; Müller, R. D.; Zahirovic, S.; Gaina, C.; Torsvik, T.; Shephard, G.; Talsma, A.; Gurnis, M.; Maus, S.; Chandler, M. (2012). "Global continental and ocean basin reconstructions since 200Ma" (PDF). Earth-Science Reviews. 113 (3): 212–270. doi:10.1016/j.earscirev.2012.03.002. Retrieved 23 October 2016. 
  • Suess, E. (1885). Das Antlitz der Erde (The Face of the Earth) (in German). 1. Leipzig, Germany: G. Freytag. Retrieved 3 September 2017. 
  • Torsvik, T. H.; Cocks, L. R. M. (2013). "Gondwana from top to base in space and time" (PDF). Gondwana Research. 24 (3): 999–1030. doi:10.1016/j.gr.2013.06.012. Retrieved 18 September 2013. 
  • Torsvik, T. H.; Voo, R. V. D. (2002). "Refining Gondwana and Pangea Palaeogeography: Estimates of Phanerozoic non‐dipole (octupole) fields" (PDF). Geophysical Journal International. 151 (3): 771–794. doi:10.1046/j.1365-246X.2002.01799.x. Retrieved 16 September 2017. 
  • Vujovich, G. I.; van Staal, C. R.; Davis, W. (2004). "Age constraints on the tectonic evolution and provenance of the Pie de Palo Complex, Cuyania composite terrane, and the Famatinian Orogeny in the Sierra de Pie de Palo, San Juan, Argentina" (PDF). Gondwana Research. 7 (4): 1041–1056. doi:10.1016/S1342-937X(05)71083-2. Retrieved 10 September 2017. 

Further reading

External links

  • Houseman, Greg. "Animation of the dispersal of Gondwanaland". University of Leeds. Retrieved 21 October 2008. 
  • Barend Köbben; Colin Reeves; Maarten de Wit. "Interactive animation of the breakup of Gondwana". ITC, University of Twente. Retrieved 16 October 2017. 
  • Graphical subjects dealing with Tectonics and Paleontology
  • Gondwana Reconstruction and Dispersion
  • The Gondwana Map Project

Retrieved from "https://en.wikipedia.org/w/index.php?title=Gondwana&oldid=806231865"
This content was retrieved from Wikipedia : http://en.wikipedia.org/wiki/Gondwana
This page is based on the copyrighted Wikipedia article "Gondwana"; it is used under the Creative Commons Attribution-ShareAlike 3.0 Unported License (CC-BY-SA). You may redistribute it, verbatim or modified, providing that you comply with the terms of the CC-BY-SA