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The Classical European Glacial Stages: Correlation with Deep-Sea Sediments View metadata, citation and similar papers at core.ac.uk brought to you by CORE provided by UNL | Libraries University of Nebraska - Lincoln DigitalCommons@University of Nebraska - Lincoln Transactions of the Nebraska Academy of Sciences and Affiliated Societies Nebraska Academy of Sciences 1978 The Classical European Glacial Stages: Correlation with Deep-Sea Sediments George Kukla Columbia University Follow this and additional works at: https://digitalcommons.unl.edu/tnas Part of the Life Sciences Commons Kukla, George, "The Classical European Glacial Stages: Correlation with Deep-Sea Sediments" (1978). Transactions of the Nebraska Academy of Sciences and Affiliated Societies. 334. https://digitalcommons.unl.edu/tnas/334 This Article is brought to you for free and open access by the Nebraska Academy of Sciences at DigitalCommons@University of Nebraska - Lincoln. It has been accepted for inclusion in Transactions of the Nebraska Academy of Sciences and Affiliated Societiesy b an authorized administrator of DigitalCommons@University of Nebraska - Lincoln. Transactions of the Nebraska Academy of Sciences- Volume VI, 1978 THE CLASSICAL EUROPEAN GLACIAL STAGES: CORRELATION WITH DEEP-SEA SEDIMENTS GEORGE KUKLA Lamont-Doherty Geological Observatory Of Columbia University Palisades, New York 10964 Four glacials and three interglacials, recognized by classical sea record revealed that this is not the case. In order to learn Alpine and North-European subdivisions of the Pleistocene, were cor­ the reasons for the discrepancy, we identified the type units related with continuous oxygen-isotope records from the oceans using and their boundaries at the type localities, correlated them loess sections and terraces as a link (Fig. 15). It was found that the Alpine "glacial" stages are represented by sediments formed during with the standard stratigraphic system, and tried to recognize both glacial and interglacial climates, that the classical Alpine "inter­ their true climatic characteristics. The record obtained from glacial" stages do not represent episodes of interglacial climate but the sea bottom, a region of practically uninterrupted deposi­ probably intervals of accelerated crustal movements, and that the tion which is the most complete system available, was used as physical evidence on which the North-European classical subdivision is a standard. based is misinterpreted due to lengthy gaps in the record. It is recommended to discontinue the use of classical terminol­ ogy in all interregional correlations and to base the chronostratigraphic subdivision of Pleistocene on the 0 18 record of deep-sea sediments. THE OXYGEN ISOTOPE RECORD It is believed that, as in Europe, the loesses and terraces in Ne­ braska will eventually provide the link needed for correlation of deep­ The ratio of oxygen isotopes 0 18 and 0 16 in foramini­ sea sediments with the classical American glacial stages. feral tests provides the most complete record of global climatic t t t changes known to date (Emiliani, 1955). It is ideally suited for a standard with which all other records can be compared. The isotopic variations in benthic foraminifera is controlled INTRODUCTION predominantly by fluctuations in the total amount of ice deposited on land (Shackleton and Opdyke, 1973, 1976). This There are two classical systems of the land-based Pleisto­ record is almost independent of the geographic location of cene in Europe namely the Alpine and the North-European. studied cores. It was also shown that the benthic 0 18 record Table I summarizes the principal information on their units. is closely paralleled by that of planktonic foraminifers, first Recently a new stratigraphy of Pleistocene has emerged, classi­ described by Emiliani (1955, 1958, 1966, 1972; Emiliani, fying deep-sea sediments after the isotopic composition of et al., 1961). Emiliani used it to subdivide deep-sea sediments oxygen in the calcareous shells of foraminifers. Because the in several Caribbean and North Atlantic cores into numbered latter is to a significant degree controlled by the volume of stages. His system, commonly referred to as the "oxygen iso­ land·locked ice, the deep-sea record closely relates to Pleisto­ tope stratigraphy" or "delta 0 18 stratigraphy," is now widely cene deposits on land. used by deep-sea researchers. The three Pleistocene subdivisions are climatostrati­ Piston core V28-238 can conveniently serve as a type graphic systems based on sequences of strata or geomorphic locality of the 0 18 /016 record (Shackleton and Opdyke, features with specific climatic signatures. As the gross changes 1973; Geitzenauer, et aI., 1976). It was taken from the equa­ ~f climate are globally synchronous, the classifications should torial Pacific at Long. 01 °Ol'N and Lat. 1600 29'E, from a e rather similar. water depth of 3120m. It is deposited at the Lamont-Doherty Geological Observatory of Columbia University, Palisades, Correlation of the classical land systems with the deep- New York. As seen in Figure 2 the upper 14m of the core are 57 TABLE I Type Units of the Classical Subdivisions of Pleistocene Interpreted System Interval Climate Type Unit Type Locality Reference Alpine Postglacial Temperate Wurm Glacial Low Terrace Riss-Wurm Interglacial Riss Glacial High Terrace PenckI and Mindel-Riss In terglacial Bruckner (1909) Mindel Glacial Younger Cover Iller-Lech Platte, Gravel Germany Gunz-Mindel Interglacial Gunz Glacial Older Cover Gravel 1 Donau-Gunz In terglacial Eberl (1930) Donau Glacial Donau Gravel Eberl (1930) Biber-Donau In terglacial Schaeffer (1953) Biber Glacial Highland Gravel Schaeffer (1953) ........................................................................................ North European Flandrian Temperate Marine and Brackish Netherlands Dubois (1925) Brackish deposits Weichsel Glacial End-Moraines North Germany, Poland Keilhack (1926) Eem In terglacial Marine and Vicinity of Amersfoort, Madsen (1929) Brackish deposits Netherlands Warthe Glacial End Moraines Central Germany Keilhack (1926) Holstein In terglacial Marine deposits Schleswig-Holstein Penck (1922) Elster Glacial Glacial-lacustrine Central Germany Keilhack (1926) Cromer In terglacial Marine and East Anglia, G.B. Reid (1882) Brackish deposits ••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••• •• , Of American Recent Temperate Lake, alluvial and North-Central USA For American usage: colluvial deposits Kay and Leighton on top of Wisconsin (1933) Wisconsin Glacial End Moraines Eastern Wisconsin Geikie (1894) (originally East Wisconsin) Sangamon In terglacial Black mud with Vicinity of Rochester, Leverett (1898) (alluvial clay?), Sangamon County, gununy clay (accre­ Illinois tion gley?), sand, gravel and peat, ferreto (red soil). 58 T ABLE I (Continued) Interpreted Interval Climate Type Unit Type Locality Reference ---System -- Illinoian Glacial Tills Southwestern Illinois Chamberlin (1896) (originally Illinois) Yarmouth In terglacial Sand, clay and Well in Yarmouth, Leverett (1898) peat with twigs exposure in West and bones of hare Point, Iowa on till Kansan Glacial Tills Northeastern Kansas Geikie (1894) Afton Temperate Gravel and sand, Exposures in Afton Chamberlin (1895) muck with vegetation Junction, Iowa (= organodetritic silts) Nebraskan Glacial Tills Exposures in the Shimek (1909) vicinity of Omaha, Nebraska subdivided into 22 oxygen isotopic stages numbered in order such as faunal assemblages (Ericson and Wollin, 1968; Imbrie of increasing age. Odd-numbered units are relatively deficient and Kipp, 1971), coccoliths (Ruddiman and McIntyre, 1973, in 0 18 and correlate with cold intervals characterized by in­ 1976), ice rafted detritus (Kent, et aI., 1971), and total car­ creased volume of land-based ice. The boundaries, defined by bonate content (Gardner and Hays, 1976; Kellogg, 1976). depth in the core, are placed near the level of fastest change of the isotopic ratio, mostly halfway between the neighbor­ In theory the 0 18 ratio in forams should provide an ac­ ing maxima and minima. Boundaries separating especially curate measure of past ice volume. However, the resolution of pronounced isotopic maxima from exceptionally pronounced the method is limited by a number of factors such as delay in minima were called "terminations" by Broecker and Van Donk ocean mixing, varying sedimentation rates, different sampling (\970). The segments bounded by two consecutive termina­ intervals, burrowing, redeposition of shells into younger sedi­ tions and composed of commonly two or up to four basic ment, selective dissolution, etc. (Shackleton and Opdyke, stages represent units of higher rank labeled "glacial cycles." 1976). As a result the precision of the method greatly de­ Terminations are numbered by Roman numerals and glacial creases with age, and the amplitudes of correlative peaks in cycles by capital letters in order of increasing age. different cores diverge to a significant degree. At present, the shapes of 0 18 curves, rather than the absolute values of iso­ Stage 5 was further subdivided by Shackleton (1969) topic ratios, are used for stratigraphic interpretations. Records into five substages labeled 5a to 5e in order of increasing age. of several cores must be compared before confident climato­ Substage 5e has the lowest isotopic ratio of the five. It corres­ stratigraphic correlations are made. Ponds to the minimum volume of ice and is considered to represent the last interglacial. Similarly, stage 7 was subdivided The reversal of the earth's magnetic field, K/
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