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On Glaciation of the Southern Andes with Special Reference to the Penı´Nsula De Taitao and Adjacent Andean Cordillera (,468300S)

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On Glaciation of the Southern Andes with Special Reference to the Penı´Nsula De Taitao and Adjacent Andean Cordillera (,468300S) Journal of South American Earth Sciences 15 (2002) 577–589 www.elsevier.com/locate/jsames On glaciation of the southern Andes with special reference to the Penı´nsula de Taitao and adjacent Andean cordillera (,468300s) C.J. Heusser Heusser and Heusser, 100 Clinton Road, Tuxedo, NY 10987, USA Received 1 May 2002; accepted 1 June 2002 Abstract Ice fronts in the southern Andes during late Wisconsin–Weichselian glaciation reached maxima early and late in oxygen isotope stage 2. 14 14 The first maximum occurred between 29,400 and 22,300 CyrBP, and the second is centered around 15,000 CyrBP. Glaciers at different latitudes varied in size, apparently in response to maximum levels of precipitation from the moisture-bearing southern Westerlies. Following 14 deglaciation, which was reached in the interior midlatitude cordillera earlier than 12,300 CyrBP, a late glacial readvance of Younger Dryas age is indicated by an increasing number of glacial geomorphic and paleoecological records, but it remains controversial. During stage 2, the cordillera supported a complex of ice caps and valley glaciers. On the Penı´nsula de Taitao and to the south, glaciers reaching low altitudes were evidently small compared with the large piedmont lobes that covered the sector encompassing the Regio´n de los Lagos–Isla Grande de Chiloe´ to the north. Flowing from an icecap on Taitao, valley glaciers became coalesced only locally, thereby giving rise to small piedmont lobes. Adjacent to Taitao in the Andes, where there is little studied evidence of stage 2 glaciation, the oldest dated advances appear to be late Holocene. Glaciers at this latitude, situated in the Tres Montes fracture zone at the Antarctic–Nazca–South American triple plate junction, have been subjected to tectonic activity. q 2002 Elsevier Science Ltd. All rights reserved. Keywords: Glaciation; Southern Andes; Glacial limits 1. Introduction netic measurements have revealed a range of contrasting ages for glacial drift that was believed by Caldenius (1932) Hollin and Schilling (1981), in their chapter ‘Late to be chronostratigraphic, which thus invalidates the Wisconsin–Weichselian Mountain Glaciers and Small Ice premise of correlation over vast sections of the cordillera. Caps’ in the Last Great Ice Sheets, presented an outline map A review of the latest literature presented herein seems (Fig. 1) that, despite its limitations, has served as a working timely to update the mapping and chronology of glaciation base for defining late Pleistocene glacial limits in the and assess the general character of the ice cover. The focus southern Andes. The extent of glaciation was generalized is on the most recent results of studies principally in the because of stratigraphic and chronological constraints. The northern and southern parts of the southern Andes; other reviews by Mercer (1976) and Paskoff (1977) provided the work from intervening latitudes has proved less informative. comparatively few records presenting significant data. Their An interpretation of aerial photographs of the Penı´nsula de concern regarding regional tectonism and synchrony of Taitao (Table 1) given here offers a view of glacial glaciation notwithstanding, Hollin and Schilling (1981),in conditions along the essentially data-poor Pacific coast. setting limits, relied heavily on the mapping accomplished The nearby triple junction of the South American, Nazca, in Fuego-Patagonia by Caldenius (1932). His Gotiglacial and Antarctic plates suggests a possible connection between limit south of 508S and Finiglacial limit north of 508S were tectonism and climate with regard to an unusual record of used to approximate the locations of ice margins most Taitao glacier fluctuations. In the Andes adjacent to the closely. As pointed out by Rabassa and Clapperton (1990) Penı´nsula de Taitao, tectonism also appears to have had a and Clapperton (1993), radioisotope dating and paleomag- coincident role, where glaciers coming out of the Campos de Hielo del San Valentı´n (northern part of Hielo Patago´nico E-mail address: [email protected] (C.J. Heusser). Norte, Fig. 1) have undergone significant advances. 0895-9811/02/$ - see front matter q 2002 Elsevier Science Ltd. All rights reserved. PII: S0895-9811(02)00076-7 578 C.J. Heusser / Journal of South American Earth Sciences 15 (2002) 577–589 Fig. 1. Estimated late Wisconsin–Weichselian ice margins in the southern Andes according to Hollin and Schilling (1981). Major existing icefields are shown stippled. C.J. Heusser / Journal of South American Earth Sciences 15 (2002) 577–589 579 14 Table 1 readvance between 11,400 and 10,200 CyrBP at the time Aerial photographic coverage provided by the US Army Air Force 1944/45 of the European Younger Dryas chronozone. Climatic of Penı´nsula de Taitao and adjoining Andes (Instituto Geogra´fico Militar, trends shown by paleoecological reconstructions for the Santiago, Chile) Regio´n de los Lagos–Isla Grande de Chiloe´ broadly parallel Locations, sorties, and exposures intervals of glacial advance and retreat believed to be as old as OIS 4 (Heusser et al., 1999). Brazo Norte–Brazo Nor Poniente: 456.L.(185–192) In the southernmost Andes (Fig. 1), the record produced Brazo Desague: 456.R.(186–188); 456.V.(186–189); 555.L.(79–81); by glaciers issuing principally from the Cordillera Darwin 555.R.(81–83) 0 Brazo Oriental: 456.R.(183–185) (54835 S) is the result of considerable study. A piedmont Brazo Sur Oriental: 456.L.(182–183); 456.R.(179–182); 456.V.(180– lobe during early OIS 2 after about 27,790 and before 14 183); 555.R.90 23,590 CyrBP spread northward some 200 km in the Brazo Sur: 456.L.(175–181); 456.R.(177–178); 456.V.(176–179) Estrecho de Magallanes and branched eastward into Bahı´a Laguna Elena: 456.L.(34–38); 456.V.(33–35) Inu´til (Clapperton et al., 1995). During late OIS 2, a Laguna Elena, Fiordo Newman sector: 408.L.(113–116); 408.R.(107– 114); 408.V.(109–114); 455.R.158; 456.R.(34–37) minimum date for subsequent full glacial advance in the Laguna San Rafael: 555.L.(88–92); 558.L.(32–38); 456.R.(175–176) vicinity of the outermost stand of the lobe, approximately 14 Golfo Elefantes: 555.L.(82–87); 558.L.(39–44) 175 km from the Cordillera Darwin, is 14,990 CyrBP 14 Glaciar San Quintı´n: 555.L.(93–99); 558.L.(26–31); 456.R.(173–174) (Ashworth et al., 1991); another date of 14,260 CyrBP Glaciar Gualas–Glaciar Reicher: 558.R.39 (McCulloch and Bentley, 1998) comes from a site within 100 km of the cordillera. In addition, reevaluation of the 2. Late Wisconsin–Weichselian glaciation of the chronology at Puerto del Hambre (568360S) provides a 14 southern Andes: an overview minimum date of 14,455 CyrBP (Heusser et al., 2000), invalidating older dates of 15,800, 16,590 and 16,290 14Cyr Glacial limits in various sectors of the Andes have been BP at the site (Heusser, 1983; Porter et al., 1992; McCulloch established with greater certainty over the past two decades and Bentley, 1998). The older dates are from samples following the estimate of ice margins outlined by Hollin and believed to be contaminated by Tertiary-age carbon Schilling (1981). In the process, the timing of glacial events (Heusser, 1999). Subsequent late glacial advance is 14 has reached a point at which regional correlation has bracketed by 12,010 and 10,050 CyrBP (McCulloch become increasingly implicit. At midlatitude (408350 – and Bentley, 1998). Justification for its possible Younger 428250S), special attention has been given to the Regio´n Dryas age is found in the paleoecological record at Puerto de los Lagos–Isla Grande de Chiloe´ (Fig. 1). Detailed del Hambre (Heusser et al., 2000). glacial geomorphic maps of Llanquihue drift (Andersen Traveling eastward from the Cordillera Darwin, a valley et al., 1999) record the presence of piedmont lobes that glacier in Canal Beagle (548550S) during late OIS 2 pushed westward to form a well-defined moraine belt west terminated just beyond the eastern entrance to the canal of Lago Puyehue, Lago Rupanco, and Lago Llanquihue and (Moat glaciation of Rabassa et al., 1990a). Aerial photo- the marine waterways of Seno Reloncavı´, Golfo de Ancud, graphs show the extent of the end moraine of the glacier and Golfo Corcovado. Lobe formation became accentuated along eastern Isla Navarino, on adjacent Isla Picton, and at by advances of the ice early and late in oxygen isotope stage Punta Moat on Isla Grande de Tierra del Fuego. A limiting 14 14 2 (OIS 2) between 29,400 and 22,300 CyrBP and 14,900– date of 14,640 CyrBP for the moraine comes from a point 14 14 14,550 CyrBP; an advance at 22,600–22,300 CyrBP along the canal where the ice front stood, approximately was apparently of maximum proportions in the north, 25 km from its terminal location, during recession (Heusser, whereas in the south, the maximum was reached between 1998). What Caldenius (1932) originally identified as an 14 14,900 and 14,800 CyrBP (Denton et al., 1999a,b). The end moraine on nearby Isla Gable has been shown to be a difference in size and timing of maxima at different latitudes drumlin field (Rabassa et al., 1990b). Deglaciation of Canal in the cordillera is attributed to a variable equatorward shift Beagle in proximity to the Cordillera Darwin dates to 14 in intensity of the storm systems of the southern Westerlies approximately 9000 CyrBP (Coronato, 1995). during OIS 2 (see Lamy et al., 2000). Earlier than 29,400 to Fluctuations of glaciers draining the southern part of the 14 .40,000 CyrBP, a lengthy interstade in this time frame Hielo Patago´nico Sur (Fig.
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