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Correlation and Late-Stage Deformation of Liv Group Volcanics in the Ross-Delamerian Orogen, Antarctica, from New U-Pb Ages

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Correlation and Late-Stage Deformation of Liv Group Volcanics in the Ross-Delamerian Orogen, Antarctica, from New U-Pb Ages Correlation and Late-Stage Deformation of Liv Group Volcanics in the Ross-Delamerian Orogen, Antarctica, from New U-Pb Ages Item Type Article Authors Paulsen, Timothy S.; Encarnación, John; Grunow, Anne M.; Stump, Edmund; Pecha, Mark; Valencia, Victor A. Citation Paulsen, T. S., Encarnación, J., Grunow, A. M., Stump, E., Pecha, M., & Valencia, V. A. (2018). Correlation and Late-Stage Deformation of Liv Group Volcanics in the Ross-Delamerian Orogen, Antarctica, from New U-Pb Ages. The Journal of Geology, 126(3), 307-323. DOI 10.1086/697036 Publisher UNIV CHICAGO PRESS Journal JOURNAL OF GEOLOGY Rights © 2018 by The University of Chicago. All rights reserved. Download date 01/10/2021 11:25:44 Item License http://rightsstatements.org/vocab/InC/1.0/ Version Final published version Link to Item http://hdl.handle.net/10150/627885 Correlation and Late-Stage Deformation of Liv Group Volcanics in the Ross-Delamerian Orogen, Antarctica, from New U-Pb Ages Timothy S. Paulsen,1,* John Encarnación,2 Anne M. Grunow,3 Edmund Stump,4 Mark Pecha,5 and Victor A. Valencia6 1. Department of Geology, University of Wisconsin, Oshkosh, 800 Algoma Boulevard, Oshkosh, Wisconsin 54901, USA; 2. Department of Earth and Atmospheric Sciences, St. Louis University, 3242 Lindell Boulevard, O’Neil Hall 205, St. Louis, Missouri 63108, USA; 3. Byrd Polar Research Center, Ohio State University, 108 Scott Hall, 1090 Carmack Road, Columbus, Ohio 43210, USA; 4. School of Earth and Space Exploration, Arizona State University, Tempe, Arizona 85287, USA; 5. Department of Geosciences, University of Arizona, Gould-Simpson Building, 1040 East Fourth Street, Tucson, Arizona 85721, USA; 6. School of the Environment, Washington State University, Pullman, Washington 99164-2812, USA ABSTRACT We present new zircon U-Pb isotopic data for volcanic rocks from deformed metavolcanic-sedimentary successions of the widespread Ross Supergroup in the Queen Maud Mountains, Antarctica. Zircon U-Pb analyses of Liv Group volcanic rocks thought to be Neoproterozoic in age instead have early Paleozoic ages. Zircon U-Pb analyses of five samples assigned to the Fairweather Formation have yielded 524 5 9 to 514 5 9Ma(2j) crystallization ages, whereas six samples assigned to the Taylor Formation have yielded 510 5 12 to 490 5 6Ma(2j) crystallization ages. Although these ages imply that the Fairweather Formation is generally older than the Taylor Formation, the age uncertainties show a 17-My overlap that is consistent with previous suggestions for temporal correlation of these formations. On a regional scale, Liv Group volcanism overlapped with the emplacement of ∼535–490 Ma plutonic rocks associated with the early Paleozoic Queen Maud batholith as well as igneous rocks found elsewhere along the early Paleozoic Pacific- Gondwana margin. Collectively, these igneous rocks provide plausible zircon sources for similar age detrital zircon populations found in outboard siliciclastic rocks belonging to the Leverett, Taylor, Fairweather, Greenlee, and Starshot Formations of the Queen Maud Mountains. The youngest crystallization age yielded by the deformed Taylor For- mation (∼490 Ma) assumes regional significance because it represents the youngest volcanic rock yet identified within the Ross orogen in Antarctica and provides important new evidence for latest Cambrian or younger deformation, possibly associated with orogenic collapse during slab rollback at the terminal stages of the Ross orogeny. Online enhancements: supplemental table. Introduction The late Neoproterozoic–early Paleozoic Ross- the Beacon Supergroup (Barrett 1991) in the Trans- Delamerian orogenic belt forms part of a greater col- antarctic Mountains, a major rift flank mountain range lage of igneous, sedimentary, and metamorphic rocks located on the margin of the Mesozoic-Cenozoic West that collectively comprise a subduction-related ac- Antarctic Rift system (Fitzgerald et al. 1986). Igne- cretionary belt along Gondwana’s paleo-Pacificmar- ous, sedimentary, and metamorphic rocks of the Ross gin known as the Terra Australis orogen (fig. 1; Boger orogen are of widespread interest because of their 2011). Rocks of the Ross-Delamerian orogenic belt are significance for understanding the tectonic history presently exposed unconformably beneath unmeta- of Gondwana’s paleo-Pacific margin (Stump 1992; En- morphosed Devonian-Jurassic sedimentary rocks of carnación and Grunow 1996; Grunow et al. 1996b; Goodge 1997; Goodge et al. 1993, 2002, 2004a, 2004b; Manuscript received January 9, 2017; accepted January 13, Cawood 2005; Boger 2011) and the possibility that 2018; electronically published March 13, 2018. they may offer insight into the Cambrian explosion * Author for correspondence; email: [email protected]. of life, since the sediment flux caused by erosion of [The Journal of Geology, 2018, volume 126, p. 307–323] q 2018 by The University of Chicago. All rights reserved. 0022-1376/2018/12603-0003$15.00. DOI: 10.1086/697036 307 This content downloaded from 150.135.119.092 on June 04, 2018 16:07:36 PM All use subject to University of Chicago Press Terms and Conditions (http://www.journals.uchicago.edu/t-and-c). 308 T. S. PAULSEN ET AL. Figure 1. Gondwana reconstruction showing the Ross-Delamerian orogen within the greater latest Neoproterozoic to late Paleozoic Terra Australis orogen as well as the major Precambrian cratons and mobile belts of Gondwana. Figure modified from Paulsen et al. (2016b). rocks of similar age is postulated to have seeded the The intent of this article is to present new zircon oceans with the elements required for organisms to U-Pb geochronologic data for volcanic rocks that develop hard body parts (Squire et al. 2006). These outcrop along the Shackleton and Liv Glaciers of rocks have been the subject of numerous field and the Queen Maud Mountains to better constrain petrographical studies (Stump 1995) as well as mod- the timing, extent, and relationship of magmatism, ern geochronologic and geochemical work (Encar- deposition, and deformation in this remote sector nación and Grunow 1996; Goodge and Dallmeyer of the Ross orogenic belt (fig. 1). Throughout this 1992, 1996; Goodge et al. 1993, 2001, 2002, 2004a, article, we use the 2015 International Chronostra- 2004b, 2012; Paulsen et al. 2013, 2015, 2016a, 2016b, tigraphic Chart time scale (Cohen et al. 2013 [up- 2017; Hagen-Peter et al. 2015, 2016; Hagen-Peter and dated]). Cottle 2016). Nevertheless, geochronologic studies have mostly been conducted on a reconnaissance ba- Geology of the Queen Maud Mountains sis throughout large sectors of the orogen, despite the fact that such data are important to help constrain Early work in the Queen Maud Mountains indicated the spatial-temporal patterns of magmatism related that the Ross Supergroup contained at least two to the evolution of the Ross-Delamerian orogen (Borg distinct tectonostratigraphic packages known as the and DePaolo 1991; Encarnación and Grunow 1996; Beardmore and Liv Groups (fig. 2; Stump 1995). The Curtis et al. 2004; Squire and Wilson 2005; Goodge Beardmore Group was considered to have an older et al. 2012; Hagen-Peter et al. 2015; Hagen-Peter and (Neoproterozoic) depositional age and includes green- Cottle 2016) and metamorphic-magmatic episodes as- schist facies siliciclastic rocks known as the La Gorce, sociated with Gondwana assembly (Boger and Miller Duncan, and Party Formations (Laird et al. 1971; 2004; Cawood 2005; Boger 2011) and Iapetus rifting Stump 1981, 1982, 1995). The Liv Group was consid- (Grunow et al. 1996b). ered to have a younger depositional age (Cambrian) This content downloaded from 150.135.119.092 on June 04, 2018 16:07:36 PM All use subject to University of Chicago Press Terms and Conditions (http://www.journals.uchicago.edu/t-and-c). Figure 2. A,Simplified geologic map showing intrusive, sedimentary, and metamorphic basement rocks of the Ross orogen from the central Transantarctic Mountains to the south through the Queen Maud and Horlick Mountains. There are abundant volcanic rocks in early to middle Cambrian stratigraphic packages (i.e., the Liv Group) in the Queen Maud Mountains, whereas the early to middle Cambrian stratigraphic packages (i.e., the Byrd Group) in the central Transantarctic Mountains are practically devoid of volcanic rocks. The boundary separating the Liv Group from the Byrd Group occurs west of the Shackleton Glacier. Asterisks indicate approximate locations of detrital zircon samples analyzed by previous authors for the Queen Maud and central Transantarctic Mountains. Diamonds indicate approximate locations of volcanic samples analyzed in this article (white diamonds) and by previous authors (black diamonds) for the Queen Maud and central Transantarctic Mountains. Labels 5A–Eand6A–F correlate with localities of samples analyzed in this article and their age data shown in figures 5 and 6. B, Locality of the Transantarctic Mountains (approximately the black area of the Ross orogen) as well as the area of the figure with respect to major crustal age provinces and the trace of the possible Proterozoic rift margin of East Antarctica. Figure compiled from Stump (1982), Borg and DePaolo (1994), Goodge (2007), and Goodge and Finn (2010). GF p Gambacorta Formation; Mts. p mountains; Neoprot. p Neoproterozoic; SVL p south Victoria Land; TP p Thiel Mountains porphyry; Trans. p Transantarctic. This content downloaded from 150.135.119.092 on June 04, 2018 16:07:36 PM All use subject to University of Chicago Press Terms and Conditions (http://www.journals.uchicago.edu/t-and-c). 310 T. S. PAULSEN ET AL. and contains volcanic and volcaniclastic rocks inter- The problems stemming from lack of age data are bedded with carbonate and siliciclastic rocks (Rowell highlighted by U-Pb crystallization ages obtained and Rees 1989) that include the Wyatt, Ackerman, from volcanic rocks of the Liv Group in the region of Leverett, Taylor, Fairweather, and Greenlee Forma- the Shackleton and Liv Glaciers (fig. 4). Van Schmus tions(Stump1995;Rowelletal.1997;RowellandRees et al. (1997) reported 550 5 15 and 516 5 6 Ma zir- 1989; Wareham et al. 2001). More recent paleonto- con U-Pb crystallization ages for volcanic rocks of logical and geochronologic studies (as in fig.
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