Elemental and stable isotope variations of organic matter from a terrestrial sequence containing the Cretaceous/Tertiary boundary at York Canyon, New Mexico

Schimmelmann, Arndt; DeNiro, Michael J.

doi:10.1016/0012-821x(84)90124-9

Cited by 42 publications

(36 citation statements)

References 30 publications

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“…The results of this study are also coarsely consistent with previous studies from terrestrial sediments elsewhere in the western interior of America that show d 13 C maxima immediately at, or some centimeters below, the Cretaceous-Paleogene claystone, and a negative excursion of 1.5‰-2.5‰ culminating in d 13 C minima above the Cretaceous-Paleogene claystone (Schimmelmann and DeNiro, 1984;Beerling et al, 2001;Arens and Jahren, 2002;Gardner and Gilmour, 2002;Maruoka et al, 2007;Therrien et al, 2007;Grandpre et al, 2013). In this study, the position of the d 13 C minimum occurs within the Cretaceous-Paleogene claystone at Frenchman Valley, to 5-10 cm above the Cretaceous-Paleogene claystone at Knudsen's Coulee (Fig.…”

Section: δ 13 C Record Of the Cretaceous Paleogene Coalssupporting

confidence: 91%

“…The fact that the shift is absent or lesser in magnitude in the contemporaneous benthos has been interpreted as evidence for the global reduction or shutdown of marine surface primary productivity (the so-called "Strangelove Ocean"; Hsü and McKenzie, 1985;Zachos et al, 1992) and/or a decrease in the flux of organic material from the surface to deep sea (D'Hondt et al, 1998;Alegret et al, 2012) at that time, resulting in the homogenization of the normal surface-to-depth positiveto-negative d 13 C gradient. A similar 1‰-3‰ negative shift in the d 13 C has also been identified across the Cretaceous-Paleogene boundary in organic carbon deposited in marine settings (e.g., Gilmour et al, 1987;Woolbach et al, 1990;Meyers and Simoneit, 1990;Hollander et al, 1993;Arinobu et al, 1999;Yamamoto et al, 2010) and fully terrestrial environments (Schimmelmann and DeNiro, 1984;Beerling et al, 2001;Gardner and Gilmour, 2002;Maruoka et al, 2007;Therrien et al, 2007;Grandpre et al, 2013). Because preserved organic carbon of terrestrial origin records the isotopic composition of the paleoatmosphere (Marino and McElroy, 1991;Jahren et al, 2008), the similarity of the terrestrial and marine d 13 C records has been used to argue for coupling of the atmospheric and shallow-marine carbon reservoirs through the mass extinction event (Beerling et al, 2001).…”

Section: Introductionmentioning

confidence: 85%

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A paleoclimatic and paleoatmospheric record from peatlands accumulating during the Cretaceous-Paleogene boundary event, Western Interior Basin, Canada

Jerrett

Price

Grimes

et al. 2015

Geological Society of America Bulletin

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Petrological and δ 13 C analyses were under taken on contiguous specimens of coal and intercalated minor organicrich clastic sedi ments collected from coal seams spanning the CretaceousPaleogene boundary in the Alberta and Saskatchewan portions of the Western Interior Basin. The generally high smectite content of the coal suggests that the original mires were largely small, discon nected, and rheotrophic, readily receiving abundant waterborne detrital clastic mate rial of largely volcanic origin. Nevertheless, using the distinctive claystone that marks the CretaceousPaleogene boundary as a regional datum , it is possible to correlate cycles in the vitrinite and inertinite compo sition of the coals over >500 km. Estimates of peat accumulation rates suggest that the cycles in vitrinite and inertinite composi tion represent regional, cyclic fluctuations in wildfire and oxi da tion of the peatlands and overlying canopy at a frequency of hundreds to thousands of years. The likely causes of these fluctuations were cyclic, regionalscale changes in temperature. The Cretaceous Paleogene boundary event occurred early during a phase of gradually increasing tem perature and/or decreasing rainfall, but peak wildfire and desiccation of peat occurred up to 14,000 yr later than the Cretaceous Paleogene boundary, and the mires did not experience significant water stress in the im mediate aftermath of the extinction event. A persistent, 1.5‰-3.0‰ negative δ 13 C excur sion occurs across the CretaceousPaleogene boundary, but it cannot be readily separated from four, further negative excursions later in the earliest Danian. The negative carbon isotope excursion linked to the Cretaceous Paleogene boundary began a few hundred years before the event itself, and recovery occurred within 21 k.y., and possibly in as little as just a few thousand years, consistent with recently calibrated shallowmarine δ 13 C records. Hence, the atmospheric and surface ocean carbon pools were coupled at this time. The absence of evidence for catastrophic change in the climatic regime at the time of the CretaceousPaleogene extinction in these mires supports the notion that the negative shift in atmospheric δ 13 C was brought about by changes in the δ 13 C composition of the sur face ocean. This is consistent with the greater magnitude of extinction experienced by ma rine fauna relative to the terrestrial realm.

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Section: δ 13 C Record Of the Cretaceous Paleogene Coalssupporting

confidence: 91%

Section: Introductionmentioning

confidence: 85%

A paleoclimatic and paleoatmospheric record from peatlands accumulating during the Cretaceous-Paleogene boundary event, Western Interior Basin, Canada

Jerrett

Price

Grimes

et al. 2015

Geological Society of America Bulletin

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“…A similar isotope shift was reported at several localities in the Raton Basin of New Mexico and Colorado (Holmes and Bohor, 1994;Lomax et al, 1998;Schimmelmann and DeNiro, 1984). At York Canyon, New Mexico, a ‫‰8.1מ‬ carbon isotope shift occurs 10 cm above the peak iridium enrichment (there is no clear boundary clay preserved at this locality; Schimmelmann and DeNiro, 1984). At two other localities, reversible negative carbon isotope shifts were accompanied by anomalies in sulfur isotopes, interpreted as sulfuric acid rain in the aftermath of impact (Holmes and Bohor, 1994;Lomax et al, 1998).…”

Section: K-t Boundary Carbon Isotope Shift In the Atmosphere Links Masupporting

confidence: 67%

“…At the Pyramid Butte locality in North Dakota, a shift of ‫‰8.2מ‬ was recorded 5 cm above the K-T boundary clay . A similar isotope shift was reported at several localities in the Raton Basin of New Mexico and Colorado (Holmes and Bohor, 1994;Lomax et al, 1998;Schimmelmann and DeNiro, 1984). At York Canyon, New Mexico, a ‫‰8.1מ‬ carbon isotope shift occurs 10 cm above the peak iridium enrichment (there is no clear boundary clay preserved at this locality; Schimmelmann and DeNiro, 1984).…”

Section: K-t Boundary Carbon Isotope Shift In the Atmosphere Links Masupporting

confidence: 63%

Chemostratigraphic correlation of four fossil-bearing sections in southwestern North Dakota

Arens¹,

Jahren²

2002

The Hell Creek Formation and the Cretaceous-Tertiary Boundary in the Northern Great Plains: An Integrated Continental Record Of

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A ‫‰5.1‬ to ‫‰2‬ carbon isotope shift in surface ocean dissolved inorganic carbon has been reported stratigraphically above the Cretaceous-Tertiary (K-T) boundary in the global stratotype section at El Kef, Tunisia, and in many other marine sections worldwide. Because a change in the d 13 C value of paleoatmospheric CO 2 would have accompanied the marine surface carbon isotope shift, the K-T carbon isotope anomaly can be used to diagnose and correlate the boundary in terrestrial sections as well. We use this shift and other secular variation in the carbon isotope signature from the Hell Creek and Fort Union Formations to correlate four sections in Slope County, North Dakota. At Pyramid Butte, the K-T boundary is marked by a ‫‰8.2‬ carbon isotope shift approximately 10 cm above the iridium-bearing impact clay. This shift is larger in magnitude than might be expected by plant vital effects or taphonomic variation. The Pyramid Butte carbon isotope shift allowed correlation to the Bobcat Butte (shift of ‫,)‰1.2‬ Terry's Fort Union Dinosaur (shift of ‫‰1.1‬ to ‫,)‰6.1‬ and the New Facet Boundary (shift of ‫)‰3.2‬ sections, where an iridium enrichment was not preserved. An interval of carbon isotope fluctuation marks the transition from HCII to HCIII megafloral zones in the Bobcat Butte section, suggesting that some instability in the physical environment was correlated with the observed vegetation change. These data demonstrate that carbon isotope chemostratigraphy can provide an additional line of evidence that is largely independent from taxonomic extinction for correlating fossil-bearing terrestrial sections. Chemostratigraphic interpretations may also recognize incomplete or condensed sections, which will aid interpretation of the fossils found in them.

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“…CAI: Conodont alteration index, a relative scale of maturity based on the color of preserved skeletal remains from specific marine fauna (conodonts). Compiled and modified after Tissot & Welte 1984;Murchison 1987;Teichmüller 1987;Boreham & Powell 1993;Taylor et al 1998, p. 127;Petersen 2002;Petersen et al 2000Petersen et al , 2004Sykes & Snowdon 2002;and Faiz 2004. deposition (Smith et al 1983) and for constraining paleoclimatic changes across the Cretaceous/Tertiary boundary (Schimmelmann et al 1984). Miocene type-IIS kerogens from California's Monterey Formation contain D/H variability that is correlated to changes in paleoceanographic conditions, although kerogens from the more mature Lion's Head section are enriched in D relative to less mature Naples Beach kerogens (Schimmelmann et al 2001b).…”

Section: Limitations On the Use Of D/h In Paleoenvironmental Reconstrmentioning

confidence: 99%

Hydrogen Isotopic (D/H) Composition of Organic Matter During Diagenesis and Thermal Maturation

Schimmelmann

Sessions

Mastalerz

2006

Annu. Rev. Earth Planet. Sci.

Self Cite

266

165

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Changes in the D/H ratio of sedimentary organic matter (SOM) during thermal maturation have been difficult to interpret because the effects of hydrogen exchange and kinetic fractionations are confounded in natural samples. Recent analytical developments have significantly improved our understanding of the responsible mechanisms. In this paper, we review experimental and field data that document a progressive increase in the D/H ratio of most organic hydrogen at the bulk and molecular levels, and suggest that the transfer of hydrogen from water to organic matter is the most important mechanism leading to those changes. SOM and water in natural petroleum systems approach a pseudoequilibrium D/H fractionation of about −80 to −110‰. D/H ratios of organic hydrogen can preserve quantitative information about paleoclimate throughout diagenesis, and some qualitative information through catagenesis.

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Elemental and stable isotope variations of organic matter from a terrestrial sequence containing the Cretaceous/Tertiary boundary at York Canyon, New Mexico

Cited by 42 publications

References 30 publications

A paleoclimatic and paleoatmospheric record from peatlands accumulating during the Cretaceous-Paleogene boundary event, Western Interior Basin, Canada

A paleoclimatic and paleoatmospheric record from peatlands accumulating during the Cretaceous-Paleogene boundary event, Western Interior Basin, Canada

Chemostratigraphic correlation of four fossil-bearing sections in southwestern North Dakota

Hydrogen Isotopic (D/H) Composition of Organic Matter During Diagenesis and Thermal Maturation

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