Recognizing the Albian-Cenomanian (Oae1d) Sequence Boundary Using Plant Carbon Isotopes: Dakota Formation, Western Interior Basin, USA
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Recognizing the Albian-Cenomanian (OAE1d) sequence boundary using plant carbon isotopes: Dakota Formation, Western Interior Basin, USA Darren R. GroÈcke School of Geography and Earth Sciences, McMaster University, Hamilton, Ontario L8S 4K1, Canada Gregory A. Ludvigson Kansas Geological Survey, University of Kansas, Lawrence, Kansas 66047-3726, USA Brian L. Witzke Iowa Department of Natural Resources, Geological Survey, Iowa City, Iowa 52242-1319, USA Stuart A. Robinson Department of Earth Sciences, University College London, London WC1E 6BT, UK R.M. Joeckel Conservation and Survey Division, School of Natural Resources, University of Nebraska±Lincoln, Lincoln, Nebraska 68588-0517, USA David F. Ufnar Department of Geography and Geology, University of Southern Mississippi, Hattiesburg, Mississippi 39406, USA Robert L. Ravn Aeon Biostratigraphic Services, 6501 Shale Circle, Anchorage, Alaska 99516, USA ABSTRACT To ascertain the effect of OAE1d (latest Albian) on the terrestrial Analysis of bulk sedimentary organic matter and charcoal carbon-isotope record, we collected bulk sediment and plant macro- from an Albian-Cenomanian ¯uvial-estuarine succession (Dakota fossils for organic carbon-isotope analysis from the Rose Creek Pit Formation) at Rose Creek Pit (RCP), Nebraska, reveals a negative (RCP) in the Dakota Formation, near Fairbury, Nebraska (Fig. 1). Pa- excursion of ;3½ in late Albian strata. Overlying Cenomanian lynostratigraphy places the section at RCP as late Albian to Cenoman- strata have d13C values of 224½ to 223½ that are similar to pre- ian in age (Brenner et al., 2000). A direct comparison between our d13 d13 excursion values. The absence of an intervening positive excursion terrestrial C records from RCP and the oceanic Cforam record at (as exists in marine records of the Albian-Cenomanian boundary) ODP Site 1052 (Wilson and Norris, 2001) provides better time reso- likely results from a depositional hiatus. The corresponding posi- tive d13C event and proposed depositional hiatus are concordant with a regionally identi®ed sequence boundary in the Dakota For- mation (D2), as well as a major regressive phase throughout the globe at the Albian-Cenomanian boundary. Data from RCP con- ®rm suggestions that some positive carbon-isotope excursions in the geologic record are coincident with regressive sea-level phases. We estimate using isotopic correlation that the D2 sequence bound- ary at RCP was on the order of 0.5 m.y. in duration. Therefore, interpretations of isotopic events and associated environmental phenomena, such as oceanic anoxic events, in the shallow- marine and terrestrial record may be in¯uenced by stratigraphic incompleteness. Further investigation of terrestrial d13C records may be useful in recognizing and constraining sea-level changes in the geologic record. Keywords: oceanic anoxic event, carbon isotopes, plants, sequence boundary, Albian-Cenomanian, middle Cretaceous. INTRODUCTION Carbon-isotope ratios (d13C) of bulk terrestrial organic matter and isolated individual plant fragments have recently been used to recon- struct terrestrial plant ecologies (Nguyen Tu et al., 1999), interpret iso- topic changes in atmospheric CO2 (GroÈcke et al., 1999), estimate at- mospheric pCO2 changes (Hasegawa et al., 2003), and assign terrestrial sequences with marine biostratigraphies (Hesselbo et al. 2000). Isotopic investigations of Cretaceous oceanic anoxic events (OAEs) indicate signi®cant shifts in the global carbon cycle, most notably during the early Aptian (OAE1a) and at the Cenomanian-Turonian boundary (OAE2). OAEs are characterized by relatively long-duration positive d13C excursions (Arthur et al., 1985) that are preceded by rapid neg- ative d13C excursions (Leckie et al., 2002), with the exception of OAE2. OAEs with negative d13C excursions have been documented throughout the Cretaceous (Herrle et al., 2003), but it is not yet known whether these events are global in distribution and affect, although Figure 1. Two overlapping stratigraphic sections were combined in this study of Rose Creek Pit (RCP), Nebraska. Stars represent sam- negative d13C excursions associated with OAE1a and OAE1b (Aptian- ple positions for palynological analysis. Arrow points to the D2 se- Albian boundary) are recorded in the terrestrial carbon reservoir quence boundary identi®ed by this study in carbon isotopes; cÐ (GroÈcke et al., 1999; Heimhofer et al., 2003). clay, sÐsilt, fmcЮne, medium, and coarse sand. q 2006 Geological Society of America. For permission to copy, contact Copyright Permissions, GSA, or [email protected]. Geology; March 2006; v. 34; no. 3; p. 193±196; doi: 10.1130/G21998.1; 4 ®gures. 193 d13 Figure 2. A: Cforam curve from ODP Site 1052, Blake Nose (Wilson and Norris, 2001), showing a rapid negative excursion in the late Albian followed by a positive excursion that peaks just before Albian-Cenomanian boundary. Labeled excursion segments are 1dpnÐ negative; 1dprÐrise; 1dppÐpositive; and 1dpdÐdecline. Foraminifera and nannofossil biostratigraphy is according to Wilson and Norris (2001). Solid black bar in R. appenninica zone gives the occurrence of laminated black shales. Note that initiation of the OAE1d negative d13 d13 d13 C excursion occurs at boundary between nannofossil zones CC9a and CC9b. B: Cbulk and Ccharcoal curves from Rose Creek Pit, Nebraska. Palynology is determined from bulk samples at 4.5 and 7.6 m. TOC values were determined during isotopic analysis of decar- bonated bulk sediment and show two phases of organic richness, beginning at onset of the negative d13C excursion and just prior to the isotopically identi®ed hiatus. Stratigraphic samples below 0 m were obtained from a nearby section on highway at RCP: This interval was dominated by sand and thus few charcoal samples were obtainable. lution within the Dakota Formation (Figs. 2A and 2B). Our data in- GEOLOGICAL SETTING AND METHODOLOGY dicate that the regressive phase associated with OAE1d occurred over The RCP locality has previously been described by Basinger and a period of ,0.5 m.y. and was a potential driver for paleoceanographic Dilcher (1984) and Upchurch and Dilcher (1990). On the basis of pa- phenomena (Watkins et al., 2005), such as disruption of a strati®ed lyno¯ora at RCP, Farley and Dilcher (1986) concluded that the deposit ocean and an extinction event. This result allows us to assess the im- is Cenomanian in age. Continuing studies, however, have shown that pact in the ocean-atmosphere system associated with OAE1d. the RCP locality straddles the Albian-Cenomanian stage boundary and contains the D2 sequence boundary of Brenner et al. (2000). The D2 surface unconformably separates deposits of the underlying Upper Al- bian Muddy Cycle (``J'' Sandstone) from the overlying Cenomanian- Turonian Greenhorn Cycle (``D'' Sandstone) (Weimer, 1987). Our pal- ynologic samples from 4.5 m at RCP (Fig. 1) produce de®nitive Upper Albian spores Disaltriangulisporites perplexus and Podocarpidites multesimus, along with numerous probable, but not necessarily de®n- itive Albian palynomorphs. Signi®cantly, no Cenomanian taxa are rec- ognized in our palynologic analysis of the leaf beds. Samples from 7.6 m at RCP (Fig. 1), however, produce de®nitive Lower Cenomanian forms Foveogleicheniidites confossus and Artiopollis indivisus, thereby bracketing the position of the D2 sequence boundary. Bulk sediment and macro-charcoal samples were collected throughout the 10 m section at RCP. Both bulk-sediment and charcoal samples were prepared according to the methods outlined in GroÈcke et al. (1999). Carbon-isotope values are reported in the standard delta (d) notation relative to VPDB with analytical precision better than 0.1½. Micromorphologic investigations of pedogenically modi®ed mudstones at the Albian-Cenomanian sequence boundary were carried out on thin sections cut from resin-impregnated billets, using methods and termi- nology from Bullock et al. (1985). TERRESTRIAL-MARINE CORRELATION An Albian-Cenomanian foraminiferal oceanic carbon-isotope curve from ODP Site 1052 shows a pronounced negative excursion at Figure 3. d13C of charcoal fragments versus bulk sediment for the boundary between nannofossil subzones CC9a and CC9b, ;100 Aptian-Albian from Algarve Basin, Portugal (Heimhofer et al., 2003), k.y. after the depositional onset of laminated black shales (Fig. 2A) and Rose Creek Pit, Nebraska (this study). For comparison, wood and bulk sediment samples from the Early Toarcian oceanic anoxic (Wilson and Norris, 2001). In order to use isotope stratigraphy as a d13 event (Jurassic) have been included (Hesselbo et al., 2000). Each correlative tool, we de®ne and label segments of the Cforam curve d13 point is representative of samples from same stratigraphic horizon. that describe its structure. The OAE1d Cforam curve shows a rapid, 194 GEOLOGY, March 2006 5 Figure 4. A: Photomicrographs of paleosol at D2 sequence boundary. Scale bars 0.2 mm, except for where indicated. (i) Cross-polarized light image of claystone paleosol with striated birefringent fabric. Bright birefringent streaks consist of oriented illuvial clay accumulations reworked from void coatings into matrix. Arrow indicates argillan (pedogenic clay coating). (ii) Cross-polarized light image of striated birefringent fabric (arrow) with overprinting sphaerosiderite nodules. Scale bar 5 1 mm. (iii) Plane-polarized light image of 0.01±0.02 mm pyrite framboids (arrow) within ®ne, faint yellow mottled domains of claystone. (iv) Cross-polarized light image of degraded clay in®lling (arrow)