Brandenburg phase
|
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 first significant advance of the Scandinavian inland ice into the Vistula high glacial is known as the Brandenburg phase . It dates approximately to the period 24,000 to 22,000 BC. Chr.
Naming and conceptual history
The Brandenburg phase, also known as Brandenburg's main advance , was introduced into the specialist literature in 1911 by O. Tietze as the Lissa phase (after Leszno in Poland ). Paul Woldstedt then referred to it as the Brandenburger Phase in 1925 and as the Brandenburger Stadium in 1928 to align with Alpine terminology . The morphostratigraphic term is defined by the terminal moraines of the Vistula High Glacial that penetrated the furthest south . The phase was named after the city of Brandenburg an der Havel , which the terminal moraine runs past to the south. The type region is the state of Brandenburg .
Geographical course
Starting from Schwerin in Mecklenburg-Western Pomerania , the Brandenburg Phase Ice Edge ( W1B ) moves in a south-easterly direction past Parchim to Northern Brandenburg, just a few kilometers southwest from the Frankfurt Ice Edge ( W1F ), which runs parallel to it . It then turns to the southwest, brushes against Pritzwalk , takes a south course shortly before reaching the Elbe and then roughly follows the border with Saxony-Anhalt . Brandenburg is bypassed to the south, at Potsdam there is a change of course to the southeast towards Luckenwalde . South of Berlin , the further course becomes indistinct, but remains north of the Glogau-Baruther glacial valley ( Sperenberg , Scheerenberge , Krausnicker Platte ). After crossing the southern Lieberoser Land , Polish territory is reached at Guben . Via Leszno it then goes to Konin , where the lobe of the Vistula glacier (Frankfurt phase) is encountered. The edge of the ice from the Brandenburg phase ends here, overlaid by sediments from the Frankfurt phase.
The transition to Schleswig-Holstein is not clear, but probably takes place south of Ratzeburg via Büchen to Schwanheide . From the extreme north-east of Hamburg , the edge of the ice is assigned to the Bruges advance ( qw1 ) (line Neumünster , Rendsburg , Schleswig , Flensburg ). In Denmark ( Jutland then) they published together with the Frankfurt-phase of the so-called main stagnation line ( Engl. Main Stationary Line ).
Stratigraphy and Correlation
The Brandenburg phase ( W1B ) belonging to marine isotope stage 2 ( MIS 2 ) joins the Denekamp interstadial and is in turn replaced by the Frankfurt phase ( W1F ). It correlates in Poland with the Leszno phase and in Schleswig-Holstein with the Bruges advance .
Internally, the Brandenburg phase can be broken down as follows (from young to old):
- Grunower halt
- Reicherskreuzer Halt / Saarmunder Halt
- Brandenburg main advance
- Vistula maximum advance
The Brandenburg phase correlates with the last ice age maximum 1 ( Last Glacial Maximum ) LGM-1 .
Juschus (2010) now prefers the main advance in Brandenburg with the Vistula maximum advance, which reached 2 to 12 kilometers further south and at one point even touched the northern edge of the Fläming .
Dating
For the Brandenburg phase, Marks (2002) derived a conventional radiocarbon age of <21,000 years from the last organic sediments beneath the glacial deposits; this corresponds to calibrated (with CalPal) <23,194 years BC A minimum age of 19,200 to 17,000 BC. Established Heine u. a. (2009) on boulders in the hinterland of the ice rim using the SED method. Lüthgens (2011) finds much older age with the help of optically stimulated luminescence (OSL method on single grains). He recommends the period 22,000 to 30,000 BC. BC or 32,000 BC Chr.
glaciology
The edge of the ice in the Brandenburg phase is rather indistinct, and the associated maximum advance in the Vistula can only be verified indirectly using hollow shapes in the terrain (indicator for dead ice ). Their reconstruction is based mostly on surveys Sander surfaces. Real terminal moraines or compressed terminal moraines are rarely found. This indicates a very rapid and relatively short-lived ice advance, which had to adapt to the conditions of the subsoil, which originated from the Saale glaciation.
The northern hinterland is mainly occupied by glaciofluvial deposits, the topography is also characterized by dead ice structures, kames and smaller alluvial plains.
To the south is the Glogau-Baruther glacial valley , which often absorbed the meltwater from the ice edge via a complicated runoff system.
Correlation with other ice sheets
Alps
In the Alps , the ice had built up around 28,000 BC. Reached the mountain edge and the valley glaciers began to spread in fan-shaped lobes in the foreland from the beginning of the late worm (MIS 2). After leaving their maximum position, they left steep-walled moraines, broad ridges and hilly landscapes behind. Compared to the Little Ice Age , the then head loss of (glacier) equilibrium line was ( Engl. Equilibrium Line Altitude or ELA ) at least 1200 to 1500 meters. In general, the meltback in the Alps began around 18,900 BC. A.
The Rhone Glacier, for example, was between 28,200 and 26,500 BC. On the advance, around 18,900 BC. Its moraines had stabilized and from 17,600 BC. He was definitely on the retreat. The Rhine Glacier had been around since 30,900 BC. On the advance and was between 24,010 and 23,450 BC. At a retreat stage (Schlieren stage). The complete melting then took place at the latest between 18,030 and 17,130 BC. Chr.
Laurentide ice sheet
The correlation of the Brandenburg phase with the development of the Laurentide Ice Sheet in North America is difficult due to the still uncertain dating. After a long rest in central Wisconsin, the Woodfordium began around 28,000 BC. First ice advances in the Great Lakes region , for example at Lake Superior with the Superior Lobe and at Lake Michigan with the Marengo phase , which have a radiocarbon age of 23,710 to 24,780 years or calibrated BC. Has. Further east at Lake Huron and Lake Erie , the advances were made a little later, for example at Lake Huron with the Huron praise shortly before 27,000 BC. And at Lake Erie with the Erie Lobe from 25,900 BC. The main advance of the Laurentide Ice Sheet, represented for example by the Shelby phase on Lake Michigan, is dated 19340 to 19680 carbon years, i.e. H. calibrated 21,151 to 21,561 BC Chr.
climate
Δ 18 O values obtained from benthic foraminifera show for the period 30,000 to 22,000 BC. A clear cooling trend (with an increase in values from 4.5 to around 4.8 ‰), which began around 23,000 BC. Reached a first interim minimum.
Cultural development
During the very cold Brandenburg phase evolved in Eurasia (France, southern Germany, Austria, Czech Republic, Poland, Ukraine and Siberia), the Upper Palaeolithic culture stage of Gravettiens (31,000 to 25,000 v. Chr.) With rückengestumpften blades Gravette peaks and cusps, as typical leading forms, followed by the beginning of the solutre . The boomerang (Oblazowa Cave, 24,000 years BC), textiles ( Dolní Věstonice ) and the first fired clay figurines were cultural innovations of the people living as hunters and gatherers . The cave paintings now reached its peak, accompanied by many hands negatives.
See also
Individual evidence
- ↑ 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.
- ↑ 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
- ↑ O. Juschus: The maximum advance of Weichselian inland ice on the northern edge of the Lusatian border wall and Flämings . In: Brandenburg. geowiss. Contrib . tape 17 , no. 1/2 . Cottbus 2010, p. 63-73 .
- ^ L. Marks: Last Glacial Maximum in Poland . tape 21 , 2002, p. 103-110 .
- ↑ K. Heine, inter alia: Timing of Weichselian ice marginal positions in Brandenburg (northeastern Germany) using cosmogenic in situ 10Be . In: Journal of Geomorphology NF . tape 53 , no. 4 , 2009, p. 433-454 .
- ↑ Christopher Lüthgens: The age of Weichselian main ice marginal positions in north-eastern Germany inferred from Optically Stimulated Luminescence (OSL) dating . In: Dissertation Free University of Berlin . 2011.
- ↑ O. Juschus: The young moraine south of Berlin - investigations into the young Quaternary landscape development between Unterspreewald and Nuthe . In: Dissertation at the Humboldt University in Berlin . 2001.
- ^ F. Preusser: Towards a chronology of the Late Pleistocene in the northern Alpine Foreland . In: Boreas . tape 33 , 2004, pp. 195-210 .
- ↑ O. Keller, E. Krayss: The Rhine-Linth glacier during the last glacial maximum. Part 1: Introduction: Construction and melting of the Rhein-Linth glacier in the Upper Würm . In: Quarterly journal of the Natural Research Society in Zurich . tape 150 , 2005, pp. 19-32 .
- ^ C. Schlüchter: The Swiss glacial record: a schematic summary . In: Quaternary Glaciations: Extent and Chronology Part I: Europe. Publisher = Elsevier . London 2004, p. 413-418 .
- ^ GS Lister: A 15,000-year isotopic record from Lake Zurich of deglaciation and climatic change in Switzerland . In: Quaternary Research . tape 29 , 1988, pp. 129-141 .
- ↑ a b Curry, BB u. a .: The DeKalb Mounds of northeastern Illinois: archives of deglacial history and postglacial environments . In: Quaternary Research . tape 74 , 2010, pp. 82-90 .
- ↑ LE Liesicki, ME Raymo: A Pliocene-Pleistocene stack of 57 globally distributed benthic d18O records . In: Paleoceanography . tape 20 , 2005.