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Reconstructing the Environmental Conditions Around the Silurian Ireviken Event Using the Carbon Isotope Composition of Bulk and Palynomorph Organic Matter

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Reconstructing the Environmental Conditions Around the Silurian Ireviken Event Using the Carbon Isotope Composition of Bulk and Palynomorph Organic Matter Article Volume 14, Number 1 31 January 2013 doi:10.1029/2012GC004348 ISSN: 1525-2027 Reconstructing the environmental conditions around the Silurian Ireviken Event using the carbon isotope composition of bulk and palynomorph organic matter Thijs R. A. Vandenbroucke Université Lille 1 - Sciences et Technologies, UMR 8217 du CNRS: Géosystèmes, Avenue Paul Langevin – bât. SN5, 59655 Villeneuve d’Ascq cedex, France Research Unit Palaeontology, Department of Geology, WE13-S8, Ghent University, 9000 Ghent, Belgium ([email protected]) Axel Munnecke Universität Erlangen-Nürnberg, GeoZentrum Nordbayern, Fachgruppe Paläoumwelt, Loewenichstr. 28, D-91054, Erlangen, Germany Melanie J. Leng Department of Geology, University of Leicester, Leicester, LE1 7RH, UK NERC Isotope Geosciences Laboratory, British Geological Survey, Nottingham NG12 5GG, UK Torsten Bickert MARUM, Center for Marine Environmental Sciences, Universität Bremen, D-28359 Bremen, Germany Olle Hints Institute of Geology, Tallinn University of Technology, Ehitajate tee 5, 19086 Tallinn, Estonia David Gelsthorpe The Manchester Museum, University of Manchester, Oxford Road, Manchester, M13 9PL, UK Georg Maier Universität Erlangen-Nürnberg, GeoZentrum Nordbayern, Fachgruppe Paläoumwelt, Loewenichstr. 28, D-91054, Erlangen, Germany Thomas Servais Université Lille 1 - Sciences et Technologies, UMR 8217 du CNRS: Géosystèmes, Avenue Paul Langevin – bât. SN5, 59655 Villeneuve d’Ascq cedex, France 13 [1] The carbon isotope composition (d C) of bulk organic matter and two palynomorph groups (scolecodonts and chitinozoans) from the Llandovery-Wenlock strata of Gotland (E Sweden) are compared to gain knowledge about carbon cycling in the Silurian (sub)tropical shelf environment. The d13C values of the palynomorphs are mostly lower than the d13C values of the bulk organic matter, and the d13Cvaluesof the benthic scolecodonts are lower than those of the planktonic chitinozoans. While the difference between bulk and palynomorph d13C may be in part a function of trophic state, the lower values of the scolecodonts relative to those of chitinozoans, which are assumed to live in the well-mixed water column, might imply ©2013. American Geophysical Union. All Rights Reserved. 86 Geochemistry Geophysics 3 Geosystems G VANDENBROUCKE ET AL.: d13C OF ISOLATED PALYNOMORPH GROUPS 10.1029/2012GC004348 an infaunal mode of life for the polychaetes that carried the scolecodonts. Lower d13C for the scolecodonts in the middle of the section may represent variations in primary marine productivity (supported by acritarch abundance data), oxidation of organic matter in the bottom waters, or genera effects. In general, however, trends between the three data sets are parallel, indicating similarities in the low frequency, envi- ronmentally forced controls. The d13C data show a decreasing trend from the base of the section, up to a horizon well below the base of the Upper Visby Formation. At this level, and therefore probably several 10 kyr before the d13C increase in the carbonates, the d13C organic values increase by ~1%. This perhaps is an expression of a changed composition of the bulk organic matter associated with the extinction events prior to the Llandovery-Wenlock boundary. Components: 8,200 words, 5 figures, 2 tables. Keywords: Gotland; Llandovery-Wenlock; carbon isotopes; scolecodonts; chitinozoans; bulk organic matter; trophic chain. Received 23 July 2012; Revised 27 November 2012; Accepted 29 November 2012; Published 31 January 2013. Vandenbroucke, T. R. A., A. Munnecke, M. J. Leng, T. Bickert, O. Hints, D. Gelsthorpe, G. Maier, and T. Servais (2013), Reconstructing the environmental conditions around the Silurian Ireviken Event using the carbon isotope composition of bulk and palynomorph organic matter, Geochem. Geophys. Geosyst., 14,86–101, doi: 10.1029/2012GC004348. 1. Introduction pH, pCO2, light, nutrients), preservation and dia- genesis, the inorganic C pool, and the analytical [2] Based on records of the carbon isotope compo- (e.g., acid digestion) method [e.g., Hinga et al., 13 1994; Popp et al., 1997, 1998; Laws et al., 2002; sition of marine carbonates (d Ccarb), the Late Ordovician and the Silurian represent one of the Brodie et al., 2011a, 2011b; Könitzer et al., 2012]. most dynamic intervals in the Phanerozoic. It is Despite these difficulties, Early Paleozoic global d13 characterized by several global, short-lived, posi- Corg events are widely interpreted in terms of 13 tive d Ccarb excursions with amplitudes exceeding global climate variation. Here we focus on the variety +5%, and maxima of over +10% [Munnecke et al., of sources that could constitute the bulk organic d13 2003, 2010; Bergström et al., 2009; Cramer et al., carbon that is measured for Corg in rocks of 2011]. New radiometric ages constrain the duration Llandovery-Wenlock age. Lécuyer and Paris [1997] of some of these excursions to notably less than tested the contributions of several palynomorph 13 1 Myr [Cramer et al., 2012]. The positive excur- types to the d C composition of Paleozoic or- sions are considered to be records of rapid and ganic matter. They indicated variations of up to large-scale changes in the ancient Earth’s global 4% among marine palynomorphs (in a range of carbon cycle, oceanography, and climate system; Silurian-Devonian marine sediment samples), and however, currently there is no consensus interpreta- up to 2.5% within a single sediment sample. Where tion that integrates cause-and-effect scenarios with there is evidence for a significant contribution of the totality of the stratigraphic data [Jeppsson et al., terrestrial derived organic matter, they showed a 13 1995; Bickert et al., 1997; Cramer and Saltzman, greater range in d Corg. Other studies have also 2005, 2007a; Noble et al., 2012]. Bulk organic matter shown the potential for isotope bias caused by the associated with the carbonates often has a carbon presence of noncontemporaneous carbon (i.e., 13 isotope composition (d Corg) that is covariant with reworked geological carbon) and of allochthonous 13 that of d Ccarb [e.g., Cramer and Saltzman, 2007b; components (e.g., land and fresh water derived Young et al., 2008; Noble et al., 2012]. However, plant remains in marine deposits), and the origin 13 the interpretation of d Corg can be complex because of amorphous organic matter is still debated [Paris of the various factors that influence the values, et al., 2008]. It is clear that it is important to know including varying sources of organic matter (e.g., about the composition of the different organic com- bacteria, phytoplankton, zooplankton), varying pro- ponents that contribute to the “bulk organic matter” duction rates of the organic material, growth rates of marine sediments that form sedimentary rocks if 13 and geometry of phytoplankton cells, and the poten- d Corg is to be used to make inferences about envi- tial presence of carbon concentrating mechanisms, ronmental change. Other studies have realized the properties of the ambient sea water (temperature, potential flaw in the bulk organic carbon approach. 87 Geochemistry Geophysics 3 Geosystems G VANDENBROUCKE ET AL.: d13C OF ISOLATED PALYNOMORPH GROUPS 10.1029/2012GC004348 For example, isotope variation of up to 4% in the from handpicked, organic-walled microfossils, chiti- Late Ordovician Guttenberg Carbon Isotope Excur- nozoans (egg cases of marine zooplankton) and sion (GICE) from Iowa was interpreted in terms of scolecodonts (jaws of benthic polychaete annelids). wide-spread environmental change and perturba- Chitinozoans, and likely their parent-animals, were tions of the carbon cycle, linked to organic carbon part of the epizooplankton, lived in the shallow “ ” burial and pCO2 (ascribed to the GICE in other mixed layer of the Ordovician-Silurian oceans, areas), as well as a partial local shift from normal- and thus occupied a habitat comparable to that of marine to Gloeocapsomorpha prisca-dominated the graptolites [Vandenbroucke et al., 2009, 2010a, organic matter [Pancost et al., 1999]. The GICE 2010b]. Chitinozoan animals are now widely excursion in Iowa exhibited values more than 4% accepted as metazoans (i.e., nonautothrophes), based more positive than in other places in the U.S. (e.g., on solid morphological analyses of chitinozoan Pennsylvania), and the authors (also see recommen- clusters [Paris and Nõlvak, 1999]. Chitinozoan dations by Popp et al. [1997]) suggested that one animals and graptolites have been hypothesized to way to decipher local from global effects on d13C occupy a higher trophic level than primary producers is by compound-specific (i.e., molecules or groups such as acritarchs, mainly based on inferred modern of molecules) or component-specific (i.e., in our analogues for acritarchs and parallel biodiversity case, on isolated specimens of a particular organic- trends between these groups [Servais et al., walled fossil group) isotope analyses. 2008]. Scolecodont-bearing worms, in contrast, are known to have been benthic animals living [3] A component-specific study was undertaken by close to the water-sediment interface [Eriksson Snelling et al. [2011]. They analyzed d13C of grap- tolite (Ordovician-Silurian macro-zooplankton) et al., 2004]. They are (at least) secondary consu- 13 mers, based on their advanced feeding/predatory periderm in comparison to d Corg of the enclosing whole rock, and noted that the difference between apparatus. The aim is to better understand the both signals is inconsistent over the Ordovician- contribution of the
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