Denekamp-Interstadial

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Glacial /
interglacial 		  Stadiale /
Interstadiale   		 Period (BC) 
Vistula late glacial
Younger dryas period 10,730-9,700
Alleröd Interstadial 11,400-10,730
Older dryas period 11,590-11,400
Bölling-Interstadial 11,720-11,590
Oldest dryas period 11,850-11,720
Meiendorf-Interstadial 12,500-11,850
Vistula high glacial
Mecklenburg phase 15,000-13,000
Pomeranian phase 18,200-15,000
Lascaux-Interstadial 19,000-18,200
Laugerie-Interstadial 21,500-20,000
Frankfurt phase 22,000-20,000
Brandenburg phase 24,000-22,000
Tursac Interstadial 27,000-25,500
Maisières-Interstadial 30,500-29,500
Denekamp-Interstadial 34,000-30,500
Huneborg Stadium 39,400-34,000
Hengelo Interstadial 41,300-39,400
Moershoofd Interstadial 48,700
Glinde Interstadial 51,500
Ebersdorf Stadium 53,500
Oerel-Interstadial 57,700
Vistula early glacial
Schalkholz Stadium 60,000
Odderade Interstadial 74,000
Rederstall-Stadial ?
Brörup-Interstadial ?
Amersfoort-Interstadial ?
Herning Stadium 115,000
Eem warm period
126,000

The Denekamp-Interstadial is a relatively mild period before the ice advances towards the end of the Vistula high glacial . It covers roughly the period 34,000 to 30,500 years BC. Chr.

Naming and conceptual history

The first description of the Denekamp Interstadial was made in 1967 by Thomas van der Hammen and others, who named it after the eastern Dutch town of Denekamp near the German border . The Dinkeltal functions as a type region .

Stratigraphy and Correlations

Temporal position of the Denekamp interstadial over the last 47,500 years

The Denekamp interstadial following the the Hengelo interstadial intermediary Huneborg stadial . It belongs to the marine isotope stage MIS 3 and correlates with the Dansgaard-Oeschger events DO6 and DO7 . The DO5 ( Maisières interstadial ) then marks the transition to Eisaufbauphase ( engl. Ice build-up ) of the last glacial maximum .

In the pollen analysis , the Denekamp interstadial corresponds to pollen levels XIII and XIV.

The Denekamp interstadial is not a uniform interstadial and so van der Hammen (1995) divided it into two interstadials, Denekamp I and Denekamp II , which correlate with DO7 and DO6. Denekamp I can be assigned to the Greenland Interstadial GI-7 and Denekamp II to the GI-6 . These two interstadials are separated from each other by a relatively brief cold relapse.

In archeology , Denekamp I correlates with the Quinçay-Interstadial and Denekamp II with the Arcy-Interstadial and Stillfried B in the Danube region. The Châtelperronien came to an end in the Quinçay Interstadial ( Aurignacien 1 ) . The Arcy-Interstadial can be equated with the Aurignacien 2 and Aurignacien 3a.

The Denekamp-Interstadial has different regional equivalents - in Norway it is called Ålesund-Interstadial , in Denmark as Sejerø-Interstadial , in Kattegatraum as Sandnes-Interstadial , in Finland / Russia as Gniew-Interstadial , in Russia as Dunayevo-Interstadial or known as Bryansk-Interstadial (with paleo-soil development ), in Western Siberia as Upper Karginsky-Interstadial (English Karginian interstadial ) and in Central Siberia as Lipov-Novoselov-Interstadial . In North America it is known as the Plum Point Interstadial and in the West Coast area it is known as the Olympic Interstadial .

geology

The profile at the type locality shows a silt mud in an upper layer of clay that can turn into peat in the area . Comparable organogenic deposits from this period have been found in several locations in the Netherlands. However, since these profiles can not be clearly characterized by pollen analysis , they must be correlated using radiocarbon dating. In neighboring countries, too, organic sites with suitable radiocarbon ages are now being added to the Denekamp Interstadial.

Wolfgang Schirmer (2012) was able to record a very complete profile through the last glacial loess with interstadial corresponding soil horizons at the Schwalbenberg site near Remagen on the Middle Rhine . Two Cambisole from the Sinzig subformation (levels S 2 and S 3) belonging to the Ahrgau Formation could be assigned to Denekamp I and Denekamp II. The dating for S 2 was 31,300 BC. And for S 3 30,700 BC. Chr.

Even more complete profiles can be found in Molodova ( Ukraine ), in the Eastern Carpathian Loess near Mitoc-Malu Galben ( Romania ) and in the Siberian locality Kurtak .

Dating

The Denekamp-Interstadial in the period 20 to 40 ka BP

Van der Hammen received the first radiocarbon dates in the type region in 1971, which indicated an uncalibrated age of 29,300 ± 300 and 30,100 ± 300 years. Calibrated (with CalPal) this corresponds to 31,741 ± 366 and 32,368 ± 224 v. After further dating by other authors, the general consensus for the Denekamp Interstadial now advocates the period 32,000 to 28,000 radiocarbon years, ie calibrated 34,069 to 30,524 BC. Chr.

Critical objection

The generally widely scattered data on organogenic layers of the outgoing Vistula high glacial show a relatively weak accumulation in the Netherlands for the period of the Denekamp interstadial. Vandenberghe and van Huissteden (1989) therefore see these locations only as local formations that were undoubtedly deposited in edaphically favorable places, but do not necessarily allow conclusions to be drawn about a general improvement in the climate. It is therefore questionable whether the Denekamp can be viewed as an outright interstadial .

Environmental parameters

The minima of the δ 18 O values , measured on the Greenland ice cores GISP 2 and NGRIP , declined slightly during the Denekamp interstadial, they lost almost 2 ‰ SMOW . The superimposed warm phases, however, brought increases by 5 ‰ SMOW (from −43 ‰ to −38 ‰ SMOW). The δ 13 C values show an analogous development, they oscillate with 2 ‰ VPDB from −7.5 ‰ to −9.5 ‰ VPDB ( stalagmite data from the northern Turkish Sofular Cave and the French Villars Cave ).

climate

The marine isotope stage 3 generally shows increasing (but decreasing in ice cores) δ 18 O values in benthic organisms , ie there was a clear cooling trend during its course. However, this cooling trend is overlaid by the two DO warm phases, with DO7 at least causing the annual temperatures to increase by 6 ° C and DO6 slightly above 4 ° C. In line with the cooling trend, there was a steady build-up of ice masses, which was only slightly influenced by the warm phases. Based on a minimum value of 3 billion cubic kilometers at the beginning of the interstadial, around 4.3 billion cubic kilometers were reached towards the end. However, large parts of Scandinavia , such as Denmark , all of Finland and southern and central Sweden, remained ice-free .

vegetation

In the north German lowlands, the steppe of the preceding Huneborg stadium (Stadial XIV (WG)) gave way to a tundra or a strauchtundra, recognizable by dwarf birch pollen ( Betula nana ), during the humid-temperate Denekamp interstadial . The widespread distribution of the sour grass family (Cyperaceae) is striking . In general, the Denekamp-Interstadial in Central Europe is characterized during the warm phases by increasing, but still quite sparse tree growth ( pine , birch and juniper ), interspersed with occasional thermophilic taxa such as hazel , oak and linden . Grasses and cyperacea prevailed in the soil vegetation with isolated aquatic plants ( water lily plants and bulrush plants ) and rare steppe dwellers such as artemisia , meadow rue , sun rose and foxtail plants .

fauna

According to Markova et al. (2013), the mammoth and woolly rhinoceros were most widespread during the Denekamp Interstadial.

Cultural development

In southern Europe , the Upper Paleolithic cultural stage of Protoaurignacia (around 38,000 to 32,000 BC) had just come to an end. In Central Europe , south-western France , Asturias and central Italy to it then the developed Aurignacian ancien (32,000 to 29,000 v. Chr.). Sites of the Aurignaciens are Willendorf II (location 4, dated 32,060 to 31,700 radiocarbon years, 34,130 to 33,698 BC) and Walou 9 near Liège in Belgium , dated 29,800 to 27,800 radiocarbon years BP (32,200 to 30,345 BC).

In Eastern Europe , the Moustérien in the west of the Crimea ( Kabazi II and Kabazi V) survived until 30,000 radiocarbon years or 32,332 BC. The micoquia was also found in the Crimea as far as the Denekamp-Interstadial ( Buran-Kaya and Kabazi V - location III / 1A). The Szeletien ( Eastern Szeletien ) reached in Buran-Kaya III until the beginning of the interstadial 34,069 years ago.

Towards the end of the Denekamp Interstadial, from around 32,000 BC. Already the Gravettien - found sites are the Geißenklösterle near Schelklingen , dated 29,220 to 26,540 radiocarbon years or 31,721 to 29,367 BC. Chr., Willendorf II position 5, dated 30,500 radiocarbon years or 32,616 BC. BC, Maisières Canal near Mons in Belgium, dated 28,240 to 27,965 radiocarbon years or 30,700 to 30,498 BC. BC and La Vigne-Brun near Roanne in France .

The people of that time, still co-existing Neanderthals and anatomically modern people ( Homo sapiens ), lived as hunters and gatherers . Typical flint shapes are keel scrapers and Dufour lamellas, and Aurignac tips were used for hunting . The first appearance of small works of art made of mammoth ivory (e.g. female statuettes ), musical instruments ( bone flutes , cave rock 33,000 BC) and cave paintings ( Chauvet cave 31,000 to 30,000 BC) is characteristic of this period.

See also

Individual evidence

  1. ↑ Thomas Litt, Achim Brauer , Tomasz Goslar, Josef Merkt, Krystyna Bałaga, Helmut Müller, Magdalena Ralska-Jasiewiczowa, Martina Stebich, Jörg FW Negendank: Correlation and synchronization of Lateglacial continental sequences in northern central Europe based on annually laminated lacustrine sediments. In: Quarternary Science Reviews. vol. 20, No. 11, May 2001, pp. 1233-1249.
  2. ↑ For the sake of standardization, the age data for the climatic stages of the Vistula Late Glacial were converted to v. With the dendrochronological and warven chronological data, the reference point is the year 1950, ie 1950 years have to be subtracted to get BC. Chr. Indications to receive. The ice core data, on the other hand, relate to the reference year 2000. The age information from the Vistula high glacial is the approximate start of the corresponding time interval vh
  3. ↑ T. Van der Hammen, inter alia: Stratigraphy, climatic succession and radiocarbon dating of the Last Glacial in the Netherlands . In: Geologie en Mijnbouw . tape 46 , 1967, p. 79-95 .
  4. ↑ JAA Bos, ao: Abrupt climatic events during OIS-3 recorded in terrestrial sediments in the Netherlands: a multi-proxy approach . In: Geophysical Research Abstracts . tape 1 , 2009.
  5. ^ T. Van der Hammen: The Dinkel Valley revisited: pleniglacial stratigraphy and global climatic change. Neogene and Quaternary Palaeoecology: a farewell to Waldo H. Zagwijn . In: GFW Herngreen, L. van der Valk (ed.): Mededelingen Rijks Geologische Dienst . tape 52 , 1995, pp. 343-355 .
  6. ↑ W. Schirmer: Rhine loess at Schwalbenberg II - MIS 4 AND 3 of . In: Quaternary Science Journal . tape 61 , no. 1 , 2012, p. 32-47 , doi : 10.3285 / e.g. 61.1.03 .
  7. ↑ T. Litt, among other things: Stratigraphic terms for the Quaternary of the north German glaciation area . In: Ice Age and the Present / Quaternary Science Journal . tape 56 , no. 1–2 , 2007, pp. 7-65 ( quaternary-science.publiss.net ). quaternary-science.publiss.net ( Memento of the original from February 5, 2015 in the Internet Archive ) Info: The archive link was inserted automatically and has not yet been checked. Please check the original and archive link according to the instructions and then remove this notice.  @1@ 2Template: Webachiv / IABot / quaternary-science.publiss.net
  8. ^ A. Svensson, inter alia: A 60,000 year Greenland stratigraphic ice core chronology . In: Clim. Past Discuss. tape 4 , 2008, p. 47-57 .
  9. ↑ D. Fleitmann, inter alia: Timing and climatic impact of Greenland interstadials recorded in stalagmites from northern Turkey . In: Geophysical Research Letters . tape 36 , 2009, doi : 10.1029 / 2009GL040050 .
  10. ↑ Liesicki, LE and Raymo, ME: A Pliocene-Pleistocene stack of 57 globally distributed benthic d18O records . In: Paleoceanography . tape 20 , 2005.
  11. ^ Shawn J. Marshall and Michelle R. Koutnik: Ice sheet action versus reaction: Distinguishing between Heinrich events and Dansgaard-Oeschger cycles in the North Atlantic . In: Paleoceanography . 21, PA2021, 2006, doi : 10.1029 / 2005PA001247 .
  12. ↑ B. Bosselin, F. Djindjian: Un essai de reconstitution du climat entre 40,000 BP and 10,000 BP à partir de séquences polliniques de tourbières et de carottes océaniques et glaciaires à haute résolution . In: Archeologia e Calcolatori . tape 13 , 2002, p. 275-300 ( soi.cnr.it [PDF]).
  13. ↑ Markova, AK et al.: New data on changes in the European distribution of the mammoth and the woolly rhinoceros during the second half of the Late Pleistocene and the early Holocene . In: Quaternary International . tape 292 , 2013, pp. 4-14 .
  14. ^ D. Richter, J. Waiblinger, WJ Rink, GA Wagner: Thermoluminescence, Electron Spin Resonance and 14C-dating of the Late Middle and Early Upper Palaeolithic Site of Geißenklösterle Cave in Southern Germany . In: Journal of Archaeological Science . tape 27 , 2000, pp. 71-89 .
  15. ^ S. Pirson, inter alia: Chronostratigraphic context of the Middle to Upper Palaeolithic transition: Recent data from Belgium . In: Quaternary International . tape 259 , 2012, p. 78-94 .
  16. ↑ M. Digan: New technological and economic data from La Vigne-Brun (unit KL19), Loire: a contribution to the identification of early Gravettian lithic technological expertise . In: Quaternary . tape 55 , 2008, p. 115-125 .