New detrital zircon age and trace element evidence for 1450 Ma igneous zircon sources in East Antarctica

Accepted Manuscript New detrital zircon age and trace element evidence for 1450 Ma igneous zircon sources in East Antarctica Timothy Paulsen, Chad Deering, Jakub Sliwinski, Olivier Bachmann, Marcel Guillong PII: DOI: Reference:

S0301-9268(16)30553-8 http://dx.doi.org/10.1016/j.precamres.2017.07.011 PRECAM 4821

To appear in:

Precambrian Research

Received Date: Revised Date: Accepted Date:

25 November 2016 11 July 2017 13 July 2017

Please cite this article as: T. Paulsen, C. Deering, J. Sliwinski, O. Bachmann, M. Guillong, New detrital zircon age and trace element evidence for 1450 Ma igneous zircon sources in East Antarctica, Precambrian Research (2017), doi: http://dx.doi.org/10.1016/j.precamres.2017.07.011

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New detrital zircon age and trace element evidence for 1450 Ma igneous zircon sources in East Antarctica Timothy Paulsen1*, Chad Deering2, Jakub Sliwinski3, Olivier Bachmann3, Marcel Guillong3 1

Department of Geology, University of Wisconsin Oshkosh, Oshkosh, WI 54901, USA Department of Geological and Mining Engineering and Sciences, Michigan Technological University, Houghton, MI 49931, USA 3 Institute of Geochemistry and Petrology, Department of Earth Sciences, ETH Zurich, Zurich, 8092, CH 2

Abstract U-Pb detrital zircon age and trace element data from a Devonian sandstone sample of the Beacon Supergroup provide new evidence for 1450 Ma zircon sources in Antarctica. These grains yield a dominant 1450 Ma (Mesoproterozoic, Calymmian) age probability peak with U/Th ratios suggesting they primarily formed from magmatic processes, also consistent with the presence of grains with oscillatory zonation. Determination of zircon parent rock types using trace element proxies reveals that the zircon grains are likely predominantly derived from granitoid rocks, with subsidiary, yet significant contributions from mafic and alkaline igneous rocks. These results are consistent with a ca. 1440 Ma (Mesoproterozoic, Calymmian) granitoid glacial erratic and similar aged detrital zircon found elsewhere in the Transantarctic Mountains that suggest a continuation of the trans-Laurentian A-type granitoid belt into Antarctica and, therefore, a 1400 Ma SWEAT-like reconstruction of the continental landmasses.

Keywords: Detrital zircon; U-Pb age; trace element; rock type; supercontinent

*

Corresponding Author. Tel.: +1 920 424 7002; Fax 1 920 424 0240; Email address: [email protected]

1 Paulsen et al., New detrital zircon age and trace element data…

1. Introduction U-Pb detrital zircon age analyses yielded a surprising result when first applied to thick sequences of continental-derived sandstone found along the Pacific-Gondwana margin (Ireland et al., 1998; Goodge et al., 2002). Instead of confirming that many of these sandstone units are late Neoproterozoic (~750-650 Ma) rift to passive margin sedimentary deposits (Goodge et al., 2002; Cooper et al., 2011) - a notion that forms part of the basis from continental reconstructions in which East Antarctica was connected to Laurentia in the Late Precambrian, for example, the SWEAT (Southwest United States-East Antarctica) hypothesis (Moores, 1991; Stump, 1992) – these authors found that many of the sedimentary successions are too young and instead represent flysch derived from late Neoproterozoic−early Paleozoic (~650-480 Ma) Gondwana mobile belts (Ireland et al., 1998; Goodge et al., 2002; Myrow et al., 2002). However, these studies also discovered a subsidiary ca. 1400 Ma (Mesoproterozoic, Calymmian) zircon age population that was postulated to have been derived from proximal source rocks of the East Antarctic shield, which presently lies underneath the East Antarctic ice sheet (Fig. 1) (Goodge et al., 2002). These detrital zircon grains yielded Hf isotopic values suggestive of an origin from eroded granitoid rocks that are similar to those found in the trans-Laurentian ~1400 Ma (Mesoproterozoic, Calymmian) A-type granitoid belt (Fig. 1A) (Goodge and Vervoort, 2006; Goodge et al., 2008). The possible continuation of this granitoid belt into the East Antarctic shield assumes regional significance because it potentially provides a critical piercing point for Proterozoic supercontinental reconstructions like the SWEAT hypothesis (Dalziel, 1991; Hoffman, 1991; Moores, 1991). Support for a granitoid provenance for some of the 1400 Ma detrital zircon grains comes from the discovery of a glacially transported 1440 Ma (Mesoproterozoic, Calymmian) A-type granite cobble recovered along the edge of the East 2 Paulsen et al., New detrital zircon age and trace element data…

Antarctic ice sheet in the central Transantarctic Mountains (Fig. 1) (Goodge et al., 2008). This clast also possesses an epsilon-hafnium initial value of +7 and an epsilon-neodymium initial value of +4 making it similar to plutonic rocks within the Laurentian intrusive belt (Goodge et al., 2008). However, importantly, there is a general paucity of information about the existence of such rock types outside of the central Transantarctic Mountains. The intent of this research note is to present new detrital zircon U-Pb age and trace element data for a Devonian Beacon Supergroup sandstone sample from the south Victoria Land sector of the Transantarctic Mountains that expands the area over which significant 1450-1400 Ma (Mesoproterozoic, Calymmian) zircon age populations are known to occur (Fig. 1). We also present an analysis of trace element data from these zircon grains with the purpose of identifying the most likely source rock types within which the detrital zircon grains crystallized. The results have the potential to better inform future studies that aspire to constrain supercontinental reconstructions (e.g., Zhao et al., 2004; Goodge et al., 2008; Li et al., 2008; Li et al., 2014). The methods used for zircon separation, U-Pb age analyses, and trace element analyses are presented as supplementary text in Appendix A. Supplementary Tables 1 and 2 list the new U-Pb age and trace element analytical data for grains that yielded age analyses that are <15% discordant (by comparison of 206Pb/238U and 206Pb/207Pb ages) or <5% reverse discordant. We use the 2015 International Chronostratigraphic Chart timescale (Cohen et al., 2013) in the discussion of the results below.

3. Results Sample PRR32746 is a fine- to medium-grained sandstone collected by Anne Grunow in 1988 from the Devonian-Jurassic Beacon Supergroup on the southeast ridge of Aztec Mountain 3 Paulsen et al., New detrital zircon age and trace element data…

(-77.802°S,

160.552°E)

near

the

head

of

Taylor

Glacier

(http://research.bpcrc.osu.edu/rr/collection/object/46093). The sample was collected from the Devonian Aztec Siltstone of the Taylor Group a few meters below an unconformity that separates it from the overlying Permian Weller Coal Measures of the Victoria Group (personal communication). The Taylor Group is a sequence of Devonian siliciclastic sedimentary rocks deposited within intermontane or successor basins upon the Kukri Erosion Surface, which developed during a period of post-orogenic uplift and erosion that marked the terminal stages of the ~590-480 Ma (Neoproterozoic-Ordovician) Ross orogeny (Isbell, 1999; Goodge et al., 2004; Rossetti et al., 2011; Hagen-Peter et al., 2016). Zircon grains from the sample are typically subrounded and display oscillatory, patchy and unzoned interiors by cathodoluminescence, occasionally with xenocrystic cores (Fig. 2). The zircon population shows a polymodal age spectrum indicating derivation from an age-varied source (Fig. 3A) or from a provenance with many ages. The cumulative zircon age suite (n=195) from the sample ranges from 2847 Ma (Mesoarchean) to 514 Ma (Cambrian, Series 2). The dominant age cluster ranges from 1722–1039 Ma (Paleoproterozoic-Mesoproterozoic, Stenian; n=148). This age cluster has four peaks in age probability at 1665 Ma (n=9), 1450 Ma (n=81), 1201 Ma (n=13), and 1065 Ma (n=3). Three age clusters also occur at 983-927 Ma (Neoproterozoic, Tonian; n=3), 719-671 Ma (Neoproterozoic, Cryogenian; n=4), and 613-509 Ma (Neoproterozoic, Ediacaran-Cambrian, Series 3). These clusters have five age probability peaks at 952 Ma (n=3), 713 Ma (n=3), 688 Ma (n=3), 578 Ma (n=12), and 524 Ma (n=5). Ninety-eight percent of the U-Pb age analyses that are <15% discordant or <5% reverse discordant have U/Th ratios of <10 suggesting the zircon grains we analyzed primarily grew during magmatic processes (Rubatto, 2002; Hoskin and Schaltegger, 2003), a result also 4 Paulsen et al., New detrital zircon age and trace element data…

consistent with the presence of zircon grains with oscillatory zoned interiors (Fig. 2) (Corfu et al., 2003). CART classification of the trace element analyses (Belousova et al., 2002) from the 191 age concordant zircon grains with trace element U/Th ratios <10 yields the following protolith rock types: 145 granitoid, 19 mafic (dolerite-basalt), and 28 alkaline (7 syenite, 5 carbonatite, and 16 syenite pegmatite/nepheline syenite). Zircon classified as grains derived from granitoid rocks yield age clusters and probability peaks that are similar to the overall U-Pb zircon age data set, with a primary 1449 Ma probability peak (Fig. 4A). Zircon classified as grains derived from mafic rocks yield a single 1484 Ma (n=7) age probability peak (Fig. 4B) while those classified as carbonatite-alkaline show probability peaks at 1465 Ma (n=9), 1207 Ma (n=7), 596 Ma (n=4), and 582 Ma (n=3) (Fig. 4C). Four zircon grains (1521, 579, 528, and 519 Ma) yield metamorphic U/Th ratios (>10), but these do not give statistically significant age clusters or probability peaks (Fig. 4D).

4. Discussion and conclusion Our analysis of the Devonian sandstone sample indicates, surprisingly, that the sandstone is dominated by a ca. 1450 Ma (Mesoproterozoic, Calymmian) detrital zircon age population. This is unexpected because the erosion of granitoid rocks and their metasedimentary country rocks within the ~590-480 Ma (Neoproterozoic-Ordovician) Ross orogenic belt produced the Kukri Erosion Surface on which Devonian sedimentary rocks were deposited (Isbell, 1999). Late Neoproterozoic-early Paleozoic metasedimentary rocks of the Ross-Delamerian orogenic belt are typically dominated by 1200-900 Ma and 700-500 Ma zircon age populations (Goodge et al., 2004; Wysoczanski and Allibone, 2004; Stump et al., 2007; Cooper et al., 2011; Paulsen et al., 2015; Paulsen et al., 2016), and these rocks serve as the country rocks to ca. 565-480 Ma 5 Paulsen et al., New detrital zircon age and trace element data…

(Neoproterozoic-Ordovician) Ross age granitoid rocks in the south Victoria Land region (Fig. 3B) (Encarnación and Grunow, 1996; Hagen-Peter et al., 2015; Hagen-Peter and Cottle, 2016). Previous detrital zircon analyses of Permian-Triassic samples from the Beacon Supergroup (in the Queen Maud Mountains, central Transantarctic Mountains, and north Victoria Land; Fig. 1B) commonly yielded large 1200-900 Ma (Mesoproterozoic-Neoproterozoic) and 700-500 Ma (Neoproterozoic-Cambrian) zircon age populations that pointed to significant zircon recycling from these older rock assemblages (Elliot and Fanning, 2008; Goodge and Fanning, 2010; Elsner et al., 2013; Elliot et al., 2015). Volcanic pebbles from the basal portion of the Devonian Taylor Group in south Victoria Land yield 497-482 Ma (Cambrian, Furongian-Ordovician, Lower) crystallization ages (Wysoczanski et al., 2003). The Ross-Delamerian age granitoids and their metasedimentary country rocks, therefore, provide potential sources for the younger ca. 1200500 Ma (Mesoproterozoic-Cambrian) zircon age population within our sample. While detrital zircon analyses of late Neoproterozoic-early Paleozoic metasedimentary rocks of the RossDelamerian orogenic belt have yielded ca. 1450 Ma (Mesoproterozoic, Calymmian) zircon age populations, these tend to be subsidiary to the dominant 1200-500 Ma (MesoproterozoicCambrian) zircon age populations (Goodge et al., 2004). Three metasedimentary rocks from the central Transantarctic Mountains have yielded large 1600-1300 Ma (Mesoproterozoic, Calymmian-Ectasian) detrital zircon age populations (Goodge et al., 2002; Goodge et al., 2004), but detrital zircon age results for these samples yielded older 1171-958 Ma (Mesoproterozoic, Stenian-Neoproterozoic, Tonian) maximum depositional ages that do not preclude deposition prior to the Ross-Delamerian orogeny. Sedimentological analyses suggest deposition of the Aztec Siltstone within an alluvial plain with sandstone paleocurrent data indicating northeast-directed flow off of the Antarctic 6 Paulsen et al., New detrital zircon age and trace element data…

shield (Barrett, 1991; Bradshaw, 2013). The 1450 Ma (Mesoproterozoic, Calymmian) zircon grains found in our sandstone sample, therefore, were likely directly sourced from similar age igneous rocks of the East Antarctic shield or are recycled from sedimentary rocks in East Antarctica that contain this anomalous age population, which themselves may reflect derivation from proximal 1450 Ma (Mesoproterozoic, Calymmian) igneous source rocks. Determination of zircon parent rock types using trace element proxies reveals that the majority of zircon grains are most likely derived from granitoid rocks, similar to previous interpretations (Goodge et al., 2008). However, trace element classification also indicates the presence of a significant population of zircon grains likely derived from mafic and alkaline source rocks. Mafic igneous rocks commonly dominate large igneous provinces, which sometimes also show smaller accompanying ultramafic, alkaline, and felsic assemblages (Ernst et al., 2008; Ernst et al., 2013). Large igneous provinces emplaced on several continents from 1600-1300 Ma (Mesoproterozoic, Calymmian-Ectasian) have been associated with the break-up of the 1800-1500 Ma (Paleoproterozoic, Statherian-Mesoproterozoic, Calymmian) Nuna (Columbia) supercontinent (Ernst et al., 2008). The Hf isotopic signatures of detrital zircon grains from central Transantarctic Mountains yielded 2000-1600 Ma (Paleoproterozoic, Orosirian-Mesoproterozoic, Calymmian) depleted mantle model ages that match Proterozoic crust in southwest Laurentia and which may occur in East Antarctica (Goodge et al., 2008). Mafic and alkaline igneous rocks are associated with the ca. 1450 Ma (Mesoproterozoic, Calymmian) magmatism within the Laurentian igneous belt (Frost et al., 2002; Dewane and Van Schmus, 2007) and the new data presented herein suggest that these rock types may also comprise a part of the East Antarctic shield.

7 Paulsen et al., New detrital zircon age and trace element data…

Acknowledgements This research used a rock sample provided by the United States Polar Rock Repository. The authors thank John Veevers and Natasha Wodicka for helpful reviews that improved this manuscript. The authors acknowledge support from the Penson Endowed Professorship and Faculty Development Program at the University of Wisconsin Oshkosh and the Scientific Center for Optical and Electron Microscopy (ScopeM) of the Swiss Federal Institute of Technology ETHZ.

Appendix A. Supplementary Text Methods Heavy mineral concentrates were isolated from the <350 µm fraction of sample PRR32746. The rock sample was disaggregated using an Electro Pulse Disaggregator (EPD) followed by traditional magnetic and heavy liquid techniques at ZirChron LLC. Zircon grains from the non-magnetic fraction were handpicked under the microscope and mounted in a 1-inch diameter epoxy puck and polished using diamond paste. U-Pb geochronology of zircon grains from sample PRR32746 was conducted by laser ablation inductively coupled plasma mass spectrometry (LA-ICPMS) at the Institute of Geochemistry and Petrology, ETH Zürich. The analyses involve ablation of zircon with a 193 nm ASI Resolution 155 ArF excimer laser using a spot diameter of 29 µm. The ablated material is carried by a helium/argon mixture to the plasma source of a Thermo Element XR magnetic sector ICPMS (Thermo Fisher, Bremen, Germany) equipped with a triple detector (pulse counter, analogue and Faraday cup). Masses 202, 204, 206, 207, 208, 232, 235 and 238 were measured, although only measurements where all isotopes were detected in pulse counting mode 8 Paulsen et al., New detrital zircon age and trace element data…

were used (<5 Mcps). Analyses were obtained using 2.0 J cm-2 energy density set at 5 Hz for 30 seconds total ablation time and a total gas blank/background measurement time of 17 seconds. Data were collected in runs of 30 samples bracketed before and after by three analyses of the primary zircon reference material GJ-1 (Jackson et al., 2004) as well as secondary reference zircons 91500 (Wiedenbeck et al., 1995), Plesovice (Sláma et al., 2008) and Temora (Black et al., 2004). Data handling and reduction were performed with Iolite v2.5 (Paton et al., 2010) and VizualAge (Petrus and Kamber, 2012), respectively, producing ages and isotope ratios corrected for mass bias, instrumental drift and downhole fractionation using primary reference material. Downhole fractionation (Paton et al., 2010) was generally very similar between primary and secondary zircon reference materials, as well as samples. For each analysis, the errors in determining

206

Pb/238U result in a measurement error of

~1-2% (2σ) in the 206Pb/238U age. The errors in measurement of 206Pb/207Pb also result in ~1-2% (2σ) uncertainty in the

206

Pb/207Pb age for grains that are >1000 Ma, but are substantially larger

(1-5%) for younger grains due to low intensity of the 207Pb signal. Interpreted ages are based on 206

Pb/238U for <1000 Ma grains and on

206

Pb/207Pb for >1000 Ma grains. This division at 1000

Ma results from the increasing uncertainty of 206Pb/ 206

238

U dates and the decreasing uncertainty of

Pb/207Pb dates as a function of increasing age. Common Pb correction was not applied en masse, but common Pb was avoided in two

ways: (1) integration windows for age and isotopic ratio determination in Iolite were selected only where the 204Pb concentration was observed to be minimal to non-existent; (2) Iolite’s Live Concordia feature was used to visualize the data in real-time, whereby integration windows were set in such a way as to avoid extremely discordant values.

9 Paulsen et al., New detrital zircon age and trace element data…

Trace elements were measured together with U-Pb for sample PRR32746 in the same ablation spot. Drift correction and standardization was performed using 2 analyses of NIST-610 synthetic glass standard every 30 analyses. Zircon reference material 91500 was analyzed once in every block of samples as a secondary reference material. Drift correction and data reduction were carried out with the MATLAB-based SILLS software (Guillong et al., 2008), and trace element concentrations were normalized to a Si value of 151682 ppm (equivalent to the Si content in a grain that is 99% ZrSiO4). Individual spot analysis error is difficult to quantify, but long-term laboratory reproducibility of homogenous glass standards indicates a precision of better than 5 rel. % for element >>LLOD (lower limit of detection). Supplementary Tables 1 and 2 list the new U-Pb age and trace element analytical data for grains that yielded age analyses that are <15% discordant (by comparison of 206

206

Pb/238U and

Pb/207Pb ages) or <5% reverse discordant. Uncertainties shown in these tables are at the 2s

level, and include only measurement errors. Systematic errors on U-Pb ages are approximately 1.6% (2s) for 206Pb/238U and 0.7% (2s) for 207Pb/235U ages. The U-Pb zircon ages are shown on a probability density diagram (from Ludwig, 2003) in Fig. 3A. This diagram shows each age and its uncertainty (for measurement error only) as a normal distribution, and sum all ages into a single curve. We applied the ‘Long’ classification and regression tree analysis (CART) shown in Fig. 7 of Belousova et al. (2002), who showed that igneous parent rock type could be distinguished using zircon trace element data with >80% confidence for carbonatite (84%), syenite (100%), Ne-syenite and syenite pegmatite (93%), and dolerite (84%). Zircon grains from other granitoid rocks (65-70% SiO2, 70-75% SiO2, >75% SiO2, and larvikite, a high-k granitoid) were distinguished with a >80% confidence with further subdivision into SiO2 classes commonly 10 Paulsen et al., New detrital zircon age and trace element data…

yielding misclassification primarily into higher or lower SiO2 content and therefore lower confidence (Belousova et al., 2002). Basalt was distinguished with a 47% confidence (Belousova et al., 2002). We excluded zircon with U/Th ratios >10 (n=4) from the CART analysis because the higher ratio can develop as a consequence of metamorphism (Hoskin and Schaltegger, 2003; Gehrels et al., 2009). The probability density diagrams (Ludwig, 2003) of the four parent rock types (granitoid, mafic, alkaline, and metamorphic) are shown in Fig. 4A-D. The age ranges of clusters and age probability peaks reported below were determined using the University of Arizona LaserChron Center Age Pick program. The program yields the number of grain ages that fall within a range (not the number of analyses that make probability contributions to define the range), as well as the number of analyses that contribute to a probability peak at the 2-sigma level. Probability peaks are required to have probability contributions from three or more overlapping analyses.

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Figure Captions Fig. 1. (A) Continental reconstruction following the SWEAT hypothesis (Moores, 1991; Dalziel, 1997) showing the trans-Laurentian A-type granitoid belt (white dots) and their possible continuation into Antarctica. White dot in Antarctica shows the location of a previously discovered ca. 1440 (Mesoproterozoic, Calymmian) granitoid glacial erratic; star symbol in Antarctica shows the approximate location of the sample locality for the sandstone analyzed in this paper. Figure modified from Hoffman (1991) and Goodge et al. (2008). (B) Physiographic map of the Antarctic continent showing the location of previous discoveries of ca. 1440 Ma (Mesoproterozoic, Calymmian) granitoid glacial erratic and detrital zircon grains within the central Transantarctic Mountains. Also shown is the location of the Devonian sandstone sample that yielded a significant population of ca. 1450 Ma (Mesoproterozoic, Calymmian) detrital zircon analyzed in this paper. Light gray areas are ice shelves, whereas dark gray indicates rock outcrop. Contours are in meters. White arrow near PRR32746 sample locality shows general paleoflow to the northeast from the East Antarctic shield recorded by the Aztec Siltstone. Image

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modified

from

public

domain

NASA

figure

available

at

https://commons.wikimedia.org/wiki/File:Antarctica.svg

Fig. 2. Representative cathodoluminescence image of zircon grains with laser spots analyzed from sample PRR32746 and their U-Pb ages.

Fig. 3. (A) Probability density plot and histograms (Ludwig, 2003) of detrital zircon U-Pb ages collected from the Devonian Beacon Supergroup sandstone sample PRR32746, and (B) with respect to stacked relative age probability diagrams of 650−480 Ma U-Pb igneous rock crystallization ages (black) and pre-Devonian metasedimentary rock detrital zircon ages from the south Victoria Land region. Detrital zircon ages are compiled from Goodge et al. (2004), Stump et al. (2007), Cooper et al. (2011), and Paulsen et al. (2015). Volcanic and plutonic U-Pb crystallization ages are compiled from Rowell et al. (1993), Hall et al. (1995), Encarnación and Grunow (1996), Cooper et al. (1997), Cox et al. 2000), Cook and Craw (2001), Allibone and Wysoczanski (2002), Read et al. (2002), Mellish et al. (2002), Wysoczanski and Allibone (2004), Cottle and Cooper (2006a), Cottle and Cooper (2006b), Stump et al. (2006), Read (2010), Cooper et al. (2011), Martin et al. (2015), Hagen-Peter et al. (2015), Hagen-Peter and Cottle (2016).

Fig. 4. Probability density plot for U-Pb ages of zircon grains from sample PRR32746 classified as being derived from granitoid (A), mafic (B), alkaline (C), and metamorphic (D) parent rocks based on trace element data.

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Highlights • • •

A Devonian sandstone yielded a large 1.45 Ga detrital zircon U-Pb age population Trace element proxies point to granitoid, mafic, and alkaline igneous source rocks Data are consistent with a continuation of the Laurentian A-type magmatic belt in Antarctica

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