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The Laurentian Record of Neoproterozoic Glaciation, Tectonism, and Eukaryotic Evolution in Death Valley, California

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The Laurentian Record of Neoproterozoic Glaciation, Tectonism, and Eukaryotic Evolution in Death Valley, California The Laurentian record of Neoproterozoic glaciation, tectonism, and eukaryotic evolution in Death Valley, California Francis A. Macdonald1,†, Anthony R. Prave2, Ryan Petterson3, Emily F. Smith1, Sara B. Pruss4, Kaylyn Oates4, Felix Waechter1, Dylan Trotzuk1, and Anthony E. Fallick5 1Department of Earth and Planetary Sciences, Harvard University, Cambridge, Massachusetts 02138, USA 2Department of Earth Science, University of St. Andrews, St. Andrews KY16 9AL, Scotland/UK 3School of Earth Sciences, The University of Queensland, Brisbane QLD 4023, Australia 4Department of Geosciences, Smith College, Northampton, Massachusetts 01063, USA 5Scottish Universities Environmental Research Centre, East Kilbride G75 0QF, Scotland/UK ABSTRACT ley predate the glaciations and do not bear et al., 2011a, 2012; Brain et al., 2012; Pruss on the severity, extent, or duration of Neo- et al., 2010) and Mongolia (Bosak et al., 2011b), Neoproterozoic strata in Death Valley, proterozoic snowball Earth events. attempts at integrating Cryogenian fossil records California, contain eukaryotic microfossils globally and assessing the biological response to and glacial deposits that have been used to INTRODUCTION Neoproterozoic glaciation have been frustrated assess the severity of putative snowball Earth by the dearth of geochronological constraints, events and the biological response to extreme The Neoproterozoic Era (1000–542 Ma) wit- along with uncertainties in stratigraphic correla- environmental change. These successions also nessed a major diversifi cation of eukaryotes, tions between different fossil localities. contain evidence for synsedimentary faulting including the origin of animals (Knoll et al., Ease of accessibility and spectacular expo- that has been related to the rifting of Rodinia, 2006), and extreme swings in climate, including sure have made the Pahrump Group of Death and in turn the tectonic context of the onset of putative snowball Earth events (Hoffman et al., Valley, California (Fig. 1), an iconic record of snowball Earth. These interpretations hinge 1998; Kirschvink, 1992). The apparent coinci- Neoproterozoic environmental change. Distinct on local geological relationships and both re- dence between Neoproterozoic glacial events early Cryogenian “Sturtian” (ca. 717–662 Ma; gional and global stratigraphic correlations. and the appearance of animals in the fossil record Bowring et al., 2007; Macdonald et al., 2010b; Here, we present new geological mapping, (Erwin et al., 2011; Love et al., 2009; Macdon- Zhou et al., 2004) glacial deposits and late Cryo- measured stratigraphic sections, carbon and ald et al., 2010b; Peterson et al., 2008; Yin et al., genian “Marinoan” (ca. 635 Ma; Condon et al., strontium isotope chemostratigraphy, and 2007) has fueled speculation concerning the 2005; Hoffmann et al., 2004) glacial deposits micropaleontology from the Neoproterozoic relationships between extreme climate change are present in the Kingston Peak Formation glacial deposits and bounding strata in Death and eukaryotic evolution (Boyle et al., 2007; on the west side of Death Valley, in the Pana- Valley. These new data enable us to refi ne Costas et al., 2008; Hoffman and Schrag, 2002). mint Mountains (Miller, 1985; Petterson et al., regional correlations, both across Death Val- Alternatively, the presence of photosynthetic 2011; Prave, 1999). However, in southeastern ley and throughout Laurentia, and construct autotrophs and heterotrophs before, and their Death Valley, it has remained unclear if glacial a new age model for glacigenic strata and survival through, Neoproterozoic glaciations deposits of the Kingston Peak Formation are microfossil assemblages. Particularly, our (Corsetti et al., 2003, 2006; Olcott et al., 2005; Sturtian or Marinoan in age (Mrofka and Ken- remapping of the Kingston Peak Formation Porter and Knoll, 2000) has been argued to pre- nedy, 2011; Prave, 1999). Conversely, in south- in the Saddle Peak Hills and near the type clude a snowball Earth scenario (Corsetti, 2009; eastern Death Valley, vase-shaped microfossils locality shows for the fi rst time that glacial Moczydlowska, 2008; Runnegar, 2000). These (VSMs), fi lamentous organisms, possible algae, deposits of both the Marinoan and Sturtian interpretations are only as good as the records and cyanobacteria are present in the Pahrump glaciations can be distinguished in southeast- on which they are based. Although the micro- Group (Corsetti et al., 2003; Licari, 1978; ern Death Valley, and that beds containing fossil record from strata deposited during the Pierce and Cloud, 1979), whereas Neoprotero- vase-shaped microfossils are slump blocks Cryogenian1 glacial interlude has increased dra- zoic microfossils have not been identifi ed on the derived from the underlying strata. These matically with discoveries from Namibia (Bosak west side of Death Valley. These paleontological slump blocks are associated with multiple fi nds include a putative synglacial biota in the overlapping unconformities that developed 1The Cryogenian Period is formally defi ned from “oncolite bed” of the Kingston Peak Formation during synsedimentary faulting, which is a 850 to 635 Ma. Herein, we follow the recommenda- (Corsetti et al., 2003), but because of strati- tion of the International Geological Correlation Pro- common feature of Cyrogenian strata along gramme (IGCP) 512 Neoproterozoic stratigraphic graphic uncertainties and structural complex- the margin of Laurentia from California to subcommission, which defi nes the base of the Cryo- ity in southeastern Death Valley (Walker et al., Alaska. With these data, we conclude that all genian at the base of the oldest Neoproterozoic gla- 1986), the age of these microfossil assemblages of the microfossils that have been described cial deposit from a global glaciation. While there is has remained unclear (Hoffman and Maloof, still controversy over the possibility of pre-Sturtian, to date in Neoproterozoic strata of Death Val- ca. 750 Ma glaciations, we assume that these deposits 2003; Macdonald et al., 2010b). Stratigraphic are not global and take the onset of the Sturtian glaci- relationships have been complicated by syn- †E-mail: [email protected]. ation at 717 Ma as the base of the Cryogenian Period. depo sitional tectonism, which has left the GSA Bulletin; July/August 2013; v. 125; no. 7/8; p. 1203–1223; doi: 10.1130/B30789.1; 14 fi gures; Data Repository item 2013253. For permission to copy, contact [email protected] 1203 © 2013 Geological Society of America Macdonald et al. W117°00′ 1975), and subsequent Cambrian passive- Noonday Fm. margin development (Armin and Mayer, 1983; Pahrump Group CA study Stewart, 1970), the region experienced Permian area basement contraction and magmatism (Snow et al., 1991). SF This was followed by the Mesozoic Cordilleran exposed bedrock LV orogeny (Burchfi el et al., 1992, 1970; Snow LA and Wernicke, 1990), and Neogene extension ′ D e a t h V a l l e y W116°00 accommodated by breakaway detachment faults (Snow and Wernicke, 2000; Wernicke et al., Panamint Mountains 1988; Wright, 1976) and associated felsic and mafi c intrusions (Calzia and Ramo, 2000; Fleck, 1970; Wright et al., 1991). ′ Stratigraphy of the Pahrump Group N36°00 BM Crystal Spring Formation The Pahrump Group begins with the Crystal NR Spring Formation, which is 300–1000 m thick SPH Figure 9 KR and rests nonconformably on Mesoprotero- AH zoic granitic to amphibolitic gneissic basement SS SW Figure 3 (Roberts , 1982; Wright, 1968). Above this sur- face, there is a variably developed basal con- Garlock fault zone glomerate (interestingly, this unit is dominated SH by light-colored meta-quartzite clasts rather than 20 km gneissic ones) that is overlain by purple to violet quartzite and shale, followed by a thick (many W117°00′ W116°00′ tens of meters) stromatolitic dolostone and then Figure 1. Simplifi ed geological map of the Pahrump Group and a cherty mudstone and fi ne-grained quartzite Noonday Formation in Death Valley. BM—Black Mountains, SS— unit (Roberts, 1982). The 1.08 Ga diabase sills Southern Ibex Hills (Saratoga Springs), SPH—Saddle Peak Hills, (Heaman and Grotzinger, 1992) intrude these SW—Sperry Wash, NR—Nopah Range, AH—Alexander Hills, strata, generating hornfels and talc (Wright, KR—Kingston Range, SH—Silurian Hills; CA—California, SF— 1968). The lower Crystal Spring Formation is San Francisco, LA—Los Angeles, LV—Las Vegas. unconformably overlain by the upper Crystal Spring Formation, which is a mixed siliciclastic- carbonate succession that is ~100–650 m thick, succession with multiple overlapping uncon- siliciclastic succession exposed across south- and is not intruded by the diabase. formities, many redeposited beds, and large eastern Death Valley and the Panamint Moun- lateral facies changes. Here, we present new geo- tains (Hazzard, 1937; Hewett, 1940, 1956; Beck Spring Dolomite logical mapping, measured stratigraphic sections, Noble, 1934; Wright et al., 1974). Upwards, it The contact between the upper Crystal Spring carbon and strontium isotope chemo stratigraphy, consists of the Crystal Spring Formation (here Formation and the Beck Spring Dolomite is tran- and microfossil discoveries from key localities differentiated into the upper and lower Crystal sitional and conformable (Roberts, 1982), and in southeastern Death Valley (Fig. 1). These data Spring Formation), the Beck Spring Dolomite, it is placed at the base of the fi rst well-defi ned, allow us to unify Neoproterozoic records across and the Kingston Peak Formation (Fig.
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