Calibration of a Conodont Apatite-Based Ordovician 87Sr/86Sr Curve to Biostratigraphy and Geochronology: Implications for Stratigraphic Resolution
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Geological Society of America Bulletin, published online on 30 June 2014 as doi:10.1130/B31038.1 Calibration of a conodont apatite-based Ordovician 87Sr/86Sr curve to biostratigraphy and geochronology: Implications for stratigraphic resolution Matthew R. Saltzman1,†, Cole T. Edwards1, Stephen A. Leslie2, Gary S. Dwyer3, Jeffrey A. Bauer4, John E. Repetski5, Anita G. Harris5, and Stig M. Bergström1 1School of Earth Sciences, Ohio State University, Columbus, Ohio 43210, USA 2Department of Geology and Environmental Science, James Madison University, Harrisonburg, Virginia 22807, USA 3Division of Earth and Ocean Sciences, Nicholas School of the Environment, Duke University, Durham, North Carolina 27708, USA 4Department of Natural Sciences, Shawnee State University, Portsmouth, Ohio 45662, USA 5U.S. Geological Survey, Reston, Virginia 20192, USA ABSTRACT rates of fall in 87Sr/86Sr at a maximum reso- stratigraphic correlation or radiometric age lution of ~0.5–1.0 m.y. Links between the uncertainties (Veizer et al., 1997; McArthur and The Ordovician 87Sr/86Sr isotope sea- increased rate of fall in 87Sr/86Sr beginning Howath, 2004; McArthur et al., 2012). water curve is well established and shows in the mid-late Darriwilian (Phragmodus po- The general structure of the 87Sr/86Sr seawater a decreasing trend until the mid-Katian. lonicus to Pygodus serra conodont zones) and curve for the Ordovician Period is well estab- However, uncertainties in calibration of this geologic events continue to be investigated, lished and shows falling values from ~0.7090 curve to biostratigraphy and geochronology but the coincidence with a long-term rise in near the base of the Ordovician to a minimum have made it diffi cult to determine how the sea level (Sauk-Tippecanoe megasequence of ~0.7078 in the middle Katian (Denison et al., rates of 87Sr/86Sr decrease may have varied, boundary) and tectonic events (Taconic orog- 1998; Qing et al., 1998; Shields et al., 2003; which has implications for both the strati- eny) in North America provides a plausible Young et al., 2009; McArthur et al., 2012; Fig. graphic resolution possible using Sr isotope explanation for the changing magnitude and 1A). However, the extent to which the rate of stratigraphy and efforts to model the effects 87Sr/86Sr of the riverine Sr fl ux to the oceans. fall varies during the Ordovician (Fig. 1B) is less of Ordovician geologic events. We measured well understood, and more intensive Sr isotope 87Sr/86Sr in conodont apatite in North Ameri- INTRODUCTION sampling is needed from sections that contain can Ordovician sections that are well studied index fossils or well-dated volcanic ash beds. for conodont biostratigraphy, primarily in The strontium isotopic (87Sr/86Sr) composi- The maximum rate of fall in 87Sr/86Sr has been Nevada, Oklahoma, the Appalachian re- tion of the ocean is homogeneous at any given estimated at ~5.0–10.0 × 10–5 per m.y. in the gion, and Ohio Valley. Our results indicate time in the geologic past because of the long Darriwilian and Sandbian Stages of the Middle that conodont apatite may provide an accu- oceanic residence time of strontium (~2–4 m.y.) to Late Ordovician (Shields et al., 2003; Young rate medium for Sr isotope stratigraphy relative to oceanic mixing times (~103 yr; Elder- et al., 2009). These authors linked the high rate and strengthen previous reports that point fi eld, 1986; Palmer and Edmond, 1989; Veizer, of fall to unusual tectonic activity and sea-level toward a signifi cant increase in the rate of 1989; McArthur, 1994; Davis et al., 2003). Sea- changes that affected Ordovician Sr fl uxes. fall in seawater 87Sr/86Sr during the Middle water 87Sr/86Sr varies over geologic time (Fig. Although parts of the Middle to Late Ordovi- Ordovician Darriwilian Stage. Our 87Sr/86Sr 1A) in response to changes in the magnitude of cian clearly stand out as periods of anomalously results suggest that Sr isotope stratigraphy the riverine Sr fl ux, the 87Sr/86Sr of rock types high rates of change in 87Sr/86Sr in McArthur will be most useful as a high-resolution tool being weathered on the continents, and the fl ux et al. (2012) (Fig. 1B), these same authors cau- for global correlation in the mid-Darriwilian of Sr from seafl oor hydrothermal weathering tioned that, as with all pre-Cenozoic time inter- to mid-Sandbian, when the maximum rate of (Hodell et al., 1990; Richter et al., 1992; Ingram vals, this result should be carefully examined for fall in 87Sr/86Sr is estimated at ~5.0–10.0 × 10–5 et al., 1994; Jones et al., 1994; Banner, 2004; evidence of time-scale compression (i.e., anom- per m.y. Variable preservation of conodont Waltham and Gröcke, 2006; Young et al., 2009). alously large 87Sr/86Sr rates of change that are elements limits the precision for individual Calibration of the 87Sr/86Sr curve to biostratig- mere artifacts of poorly constrained radiometric stratigraphic horizons. Replicate conodont raphy and geochronology makes it possible to age dates or biostratigraphic correlation) before analyses from the same sample differ by an use Sr isotope stratigraphy as an independent drawing conclusions about causal factors (e.g., average of ~4.0 × 10–5 (the 2σ standard de- method to correlate rocks (Burke et al., 1982; Jurassic example in Waltham and Gröcke, 2006; viation is 6.2 × 10–5), which in the best case McArthur et al., 2001). Sr isotope stratigraphy McArthur and Wignall, 2007). scenario allows for subdivision of Ordovician is commonly applied to Mesozoic and Ceno- If observed high rates of change in the time intervals characterized by the highest zoic time periods, but efforts in the Paleozoic Middle to Late Ordovician are not drastically have been hindered by a lack of abundance of diminished with improvements in radiometric †E-mail: [email protected]. well-preserved materials and uncertainty in age dates and biostratigraphic calibration, this GSA Bulletin; Month/Month 2014; v. 1xx; no. X/X; p. 1–18; doi: 10.1130/B31038.1; 12 fi gures; 1 table; Data Repository item 2014240. For permission to copy, contact [email protected] 1 © 2014 Geological Society of America Geological Society of America Bulletin, published online on 30 June 2014 as doi:10.1130/B31038.1 Saltzman et al. (2012) shown in our Figure 1A (note that McArthur et al. [2012] also utilized bulk rock data from Gao and Land, 1991; Denison et al., 1998; Young et al., 2009; and conodont data from Ebneth et al., 2001). Although well-pre- served brachiopods composed of diagenetically resistant low-Mg calcite are generally accepted as a medium for accurate measurement of 87Sr/86Sr trends in the Ordovician and else- where in the Paleozoic (e.g., Korte et al., 2006; Van Geldern et al., 2006; Brand et al., 2012), signifi cant gaps in their availability occur in parts of the Middle to Late Ordovician. Cono- dont apatite can be extracted from virtually every marine Ordovician-aged carbonate rock and tied to the global conodont biostratigraphic zonation (Fig. 3), which is the most widely used zonation in Ordovician carbonate facies (e.g., Harris et al., 1979; Bergström, 1971, 1986; Sweet, 1984; Sweet et al., 2005; Cooper and Sadler, 2012). The use of conodont apatite as an accurate and precise medium for seawater 87Sr/86Sr stratigraphy is debated in the litera- ture because of questions about the commonly observed postmortem incorporation of signifi - cant amounts of Sr, which could derive from seawater or non-seawater sources depending on pore-water conditions (e.g., Bertram et al., 1992; Kürschner et al., 1992; Cummins and Elderfi eld, 1994; Holmden et al., 1996; Ruppel et al., 1996; Ebneth et al., 1997, 2001; Veizer Figure 1. (A) Phanerozoic 87Sr/86Sr and (B) rates of change, both et al., 1997; Qing et al., 1998; Korte et al., 2003, after McArthur et al. (2012). The curve in A is the LOWESS (locally 2004; Martin and Scher, 2004; Twitchett, 2007). weighted scatterplot smoother), which is a statistical nonparametric Similar debate surrounds use of bulk rock for Sr regression method fi t to the data sources in McArthur et al. (2012). isotope stratigraphy (e.g., Gao and Land, 1991; Ordovician study interval is highlighted with gray box. Denison et al., 1998; Young et al., 2009), and we have a separate study under way to better char- acterize accuracy and precision in fossil mate- interval, which is marked by major biologi- Oklahoma, the Ohio Valley, and Appalachian rials versus bulk rock in the Ordovician using cal and climatic changes (Trotter et al., 2008; region (Figs. 2 and 3). To calculate rates of some of the same sections analyzed in the pres- Servais et al., 2010), holds great promise for change in 87Sr/86Sr, we utilize the new Geologic ent contribution (Edwards et al., 2013). Sr isotope stratigraphy. McArthur et al. (2012) Time Scale 2012 (Cooper and Sadler, 2012). Our Direct comparisons between Ordovician calculated that when rates of 87Sr/86Sr change in results, which support use of conodont apatite as conodonts and brachiopods may be used to the Phanero zoic exceed 5.0 × 10–5 per m.y. (Fig. an accurate medium for seawater 87Sr/86Sr under assess their accuracy for seawater 87Sr/86Sr 1B), the stratigraphic resolution in these time certain circumstances, strengthen the notion that measurements. The precision (reproducibil- periods can theoretically surpass 0.1 m.y. In the Ordovician Sr isotope stratigraphy is particu- ity) of these materials, which also determines Ordovician, 0.1 m.y. resolution using Sr isotope larly effective as a high-resolution correlation their effectiveness for use in Sr isotope stratig- stratigraphy likely cannot be achieved because tool in the mid-Darriwilian to mid-Sandbian raphy, can be compared with each other but also of limitations in biostratigraphy, geochronology, Stages characterized by high rates of 87Sr/86Sr with younger periods.