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Ameghiniana

versión impresa ISSN 0002-7014

Ameghiniana vol.47 no.1 Buenos Aires ene./mar. 2010

 

NOTA PALEONTOLÓGICA

West Antarctic Rift system: a possible New Zealand-Patagonia Oligocene paleobiogeographic link

Silvio Casadío1, Campbell Nelson2, Paul Taylor3, Miguel Griffin4 and Dennis Gordon5

1Universidad Nacional de La Pampa, Uruguay 151, 6300 Santa Rosa, Argentina. scasadio@cpenet.com.ar
2University of Waikato, Private Bag 3105, Hamilton 3240, New Zealand. c.nelson@waikato.ac.nz
3Natural History Museum, Cromwell Road, London SW7 5BD, United Kingdom. p.taylor@nhm.ac.uk
4Museo de La Plata, Paseo del Bosque s/n, 1900 La Plata, Argentina. miguelgriffin@aol.com
5NIWA, PO Box 14901, Kilbirnie, Wellington, New Zealand. d.gordon@niwa.co.nz

The extant marine benthic faunas in the New Zealand region and those belonging to the Magallanes and Antarctic biogeographic provinces may share a common origin dating back as far as the Early Cretaceous (Zinsmeister, 1982; Crame, 1999). These faunas have diverged ever since but the tempo and mode of this divergence remains imperfectly understood. Studies on the biogeographical affinities among the marine benthic faunas from the Southern Hemisphere point to close paleobiogeographical relationships between New Zealand, West Antarctica and southern South America after the final break-up of Gondwana (Griffin and Hünicken, 1994; Zinsmeister and Griffin, 1995; Stilwell, 2003).
The paleobiogeographical evolution of these faunas occurred in the context of the dramatic and continuous geodynamic events that led from rela-tively warm, ice-free "greenhouse" conditions to an "icehouse" state (Francis et al., 2009). Crucial oceanographic modifications took place in the Southern Hemisphere during the period between 35 and 15 Ma. These included the establishment of broad zonal belts of surface-water masses separated by oceanic fronts (Nelson and Cooke, 2001; Lagabrielle et al., 2009). These belts had a paramount role in the isolation and evolution of the marine faunas in the Southern Hemisphere (Arntz, 1999). However, paleontological evidence demonstrates that during this period paleobiogeographic connections between New Zealand and Patagonia were maintained, as shown by the presence of numerous shared taxa. Twenty two mollusk genera appearing in South American Late Oligocene-Miocene rocks are recorded also in New Zealand, but making their first appearance there in older rocks (Deminucula, Notolimopsis, Glycymeris (Glycymerula), Cyclochlamys, Gonimyrtea, Spissatella, Scalpomactra, Turia, Crosseola, Sigapatella, Trichosirius, Sassia zealta group, Ataxocerithium, Penion, Nassarius (Hima), Xymenella, Austromitra, Zeacuminia, Eoturris, Neoguraleus (Fusiguraleus), Oamaruia (Oamaruia), and Opimilda. At the same time, 16 taxa appear in South America in rocks older than those containing these taxa in New Zealand (Zygochlamys, Tiostrea, Aulacomya, Lucinoma, Antisolarium (from Valdesia), Xymene, ?Trophon, Provocator, Antimelatoma, Solemyarina, Anadara, Mytilus, Protothaca, Diloma, Argobuccinum, Fusitriton). At the same time (Late Oligocene-Early Miocene), eight genera appear in both areas (Neopanis, Austrovenus (from Ameghinomya), Cirsotrema (large species), Oamaruia (Zeadmete), Puyseguria, Cosa, Notolimea, Lamprodomina (Beu et al., 1997).
Bryozoans recorded from around the Oligocene-Miocene boundary in Patagonia are typically pan-Gondwanan. However, a recent record of a species belonging to Cinctiporidae (figure 1) -a distinctive family previously regarded as a New Zealand endemic (Boardman et al., 1992) - within the Monte León Formation (Early Miocene) cropping out in the Puerto Deseado area (47º 32' 52'S, 66º 30' 57''W), Argentina, reinforces the idea of connections between the western South Atlantic and New Zealand as late as the Early Miocene. With the exception of a doubtful occurrence in the Maastrichtian of South Africa (Boardman et al., 1992), cinctiporids were known only from the Late Paleocene-Early Eocene to Recent of New Zealand (Gordon and Taylor, 1999) before the surprising discovery of the Argentinean material.


Figure 1. Specimen GHUNLPam 28.000 from Puerto Deseado area (Argentina) belonging to the cyclostome bryozoan family Cinctiporidae hitherto considered to be endemic to New Zealand. The specimen is housed in the Departamento de Ciencias Naturales of the Universidad Nacional de La Pampa / especímen GHUNLPam 28.000 del área de Puerto Deseado (Argentina) perteneciente a un briozoo ciclostomado de la familia Cinctiporidae hasta ahora considerada endémica de Nueva Zelanda. El ejemplar se encuentra depositado en la colección del Departamento de Ciencias Naturales de la Universidad Nacional de La Pampa.

Despite the enormous distance separating New Zealand and South America during the Oligocene (15,000 km eastward from South America to New Zealand and 9,000 km from New Zealand to South America), these affinities among benthic faunas with mainly short-lived larvae have been attributed by Beu et al. (1997) largely to the action of the Antarctic Circumpolar Current, established as a consequence of the opening of Drake Passage. However, if this were true it would be difficult to explain the low dispersion rate after the Early Miocene.
Here we postulate that the paleobiogeographic connection may have been along the West Antarctic Rift system. This system underwent an episode of significant extension during the Eocene-Oligocene (Cande et al., 2000), especially evident from seismic imaging in the McMurdo Sound (Fielding et al., 2008), and at the same time the full opening (ca. 31 Ma) of the Tasmanian gateway possibly elicited the onset of a protocircum-Antarctic flow of cold waters, perhaps through a West Antarctic seaway connecting the southern Pacific and Atlantic Oceans (figure 2), a scenario advocated by Nelson and Cooke (2001). While conclusive support for this hypothesis is presently limited, information assembled during the last decade after research in McMurdo Sound is very enlightening. Boreholes CRP-2/2a and CRP-3 of the Cape Roberts Project cored approximately 1,300 m of Oligocene sediments in the Victoria Land Basin of the Ross Sea (CRST, 1999a, 1999b, 2000a, 2000b), yielding mollusks (Taviani and Beu, 2001), corals (Stolarski and Taviani, 2001), and ostracods (Dingle and Majoran, 2001) that show affinities with New Zealand and Patagonian taxa alike. Erratic boulders with giant oysters found in McMurdo Sound (albeit with no precise dating) strongly suggest the existence of great oyster reefs along the Antarctic shelf (Stilwell, 2000) similar to those described from Late Oligocene-Early Miocene successions in Patagonia (Parras and Casadío, 2005, 2006) and New Zealand (Nelson et al., 1983). These oysters built framework reefs in shallow-shelf environments, forming large biogenic concentrations exposed at many localities in Patagonia and New Zealand (figure 3).


Figure 2. Schematic paleogeographic map showing the suggested marine connections during the Oligocene. OR = oyster reefs, C = Cinctiporidae. Base map modified from Nelson and Cooke (2001), Ghidella et al. (2002) and Ghiglione et al. (2008) / mapa paleogeográfico esquemático mostrando las conexiones marinas sugeridas para el Oligoceno. OR = arrecifes ostreros, C = Cinctiporidae. Mapa base modificado de Nelson y Cooke (2001), Ghidella et al. (2002) y Ghiglione et al. (2008).


Figure 3. Oyster reefs. 1, oyster reef in the Late Oligocene-Early Miocene Centinela Formation, La Siberia, Santa Cruz, Argentina; 2, Oyster reef in the Late Oligocene-Early Miocene Te Kuiti Group, Piripiri Cave, Waitomo, New Zealand / arrecifes ostreros. 1, arrecife ostrero en la Formación Centinela (Oligoceno Tardío-Mioceno Temprano), La Siberia, Santa Cruz, Argentina; 2, Arrecife ostrero en el Grupo Te Kuiti (Oligoceno Tardío-Mioceno Temprano), Cueva Piripiri, Waitomo, Nueva Zelanda.

In conclusion, there is an accumulating body of tectonic, sedimentary and paleontological information that the West Antarctic Rift system could have afforded a principal paleobiogeographic seaway linkage between New Zealand and Patagonia in the Oligocene.

References

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Recibido: 19 de junio de 2009.
Aceptado: 18 de setiembre 2009.