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LGM) in the Southeastern Swiss Alps (Graubünden) and Its Paleoclimatological Significance

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LGM) in the Southeastern Swiss Alps (Graubünden) and Its Paleoclimatological Significance 23 — 37 Eiszeitalter u. Gegenwart 48 Hannover 1998 7 Fig. Surface geometry of the Last Glacial Maximum (LGM) in the southeastern Swiss Alps (Graubünden) and its paleoclimatological significance DURI FLORINETH*) Last Glacial Maximum, Swiss Alps, trimlines, flowdirection, modelling, paleoglaciology, paleoclimatology Abstract: Using detailed field evidence provided by gen des Eises, und die Morphologie des Felsuntergrun­ trimlines on former nunataks, erratic boulders and the des entlang der Haupt- und Seitentäler deuten darauf orientations of glacial striae, the surface geometry in the hin, daß das ehemalige Akkumulationsgebiet aus ei­ accumulation area during the Last Glacial Maximum nem Eisdom bestand. Die Eisscheide lag dabei über was reconstructed for the area of SE Switzerland and dem von Schlarignia, Cinuos-chel, Livigno und Piz Ber­ adjacent Italy. Collectively, the trends of trimline eleva­ nina eingeschlossenen Gebiet und erreichte eine mini­ tions, flowlines deduced from glacial striae and be­ male Höhe von ca. 3000 m. Diese Resultate konnten drock morphology along the longitudinal valleys and durch eine Modelliernng der Topographie dieser Eis­ their tributaries indicate that the former accumulation oberfläche mit Hilfe eines Geographischen Informati­ area consisted of an ice dome with the ice divide loca­ onssystems (GIS) bestätigt werden. ted over the area enclosed by Schlarignia, Cinuos-chel, Das Klimasignal, welches in dieser Gletschergeometrie Livigno and Piz Bernina. It attained a minimum altitude enthalten ist, wurde anschließend genutzt, um vorher­ of approximately 3000 m. Modelling the topography of sehende atmosphärische Zirkulationsmuster und die the ice surface using a Geographical Information Sy­ daraus resultierenden Hauptniederschlagsgebiete in stem (GIS) is consistent with these results. den Alpen während des letzten Hochglazials zu bestim­ The paleoclimatological signal included in this surface men. Es läßt sich daraus folgern, daß für den Aufbau geometry was used to draw conclusions about the main des Eisdomes vorwiegend Niederschläge von Südstau­ atmospheric paleocirculation patterns and to outline lagen verantwortlich waren. Die Dominanz der Süd­ the principal precipitation areas for the Alps during the staulagen ist eine direkte Folge der vorrückenden Meer­ last glaciation. It followed from this that ice build-up eisgrenze im Nordatlantik. Letztere bedingte eine Ver­ was principally related to dominating precipitation by lagerung der atmosphärischen Polarfront und der damit southerly circulation (foehn). The prevaleance of foehn verbundenen Hauptzugbahn zyklonaler Störungen um circulation most likely reflects a southward shift of the bis zu 20° südwärts. North Atlantic polar atmospheric front and of the ac­ Diese Ergebnisse korrespondieren gut mit (a) den Re­ companied storm track due to the advancing margin of sultaten globaler Zirkulationsmodelle für das LGM; (b) sea ice. Schätzungen der basalen Schubspannungen und der There exists good agreement between these assumpti­ Fliessgeschwindigkeiten für die Eiszeitgletscher; und ons and (a) results of global circulation models for the (c) mit der Interpretation von Paläowind-Indikatoren. time of the LGM; (b) estimations of basal shear stress va­ lues and flow velocities for Ice Age glaciers; and (c) in­ terpretations of paleowind indicators. Introduction [Die Oberflächengeometrie des letzteiszeitlichen Paleoglaciological reconstructions are usually do­ Maximums (LGM) in den südöstlichen ne by means of mapping geological and geomor- schweizer Alpen (Graubünden) und ihre phological depositional features in the areas be­ paläoklimatologische Bedeutung] low the equilibrium line altitude (ELA), and of Kurzfassung: Anhand detaillierter Feldbefunde, wie erosional features in the former accumulation z.B. Schliffgrenzen an ehemaligen Nunatakern, der Ver­ area. Detailed field evidence in the former ablati­ teilung erratischer Blöcke und der Orientierung von Gletscherschrammen, wurde die Oberflächengeome­ on area and recent progress in the field of com­ trie des Akkumulationsgebietes des letzteiszeitlichen puter technology has led to increasing interest in Maximums im Gebiet Südostschweiz und Norditalien numerical modelling and reconstructing Pleisto­ rekonstruiert. Der Höhenverlauf der Schliffgrenzen, die cene Alpine glaciers, especially in connection aus den Striemungsdaten abgeleiteten Fließbewegun- with the following questions: (a) the maximal ex­ tent of the former piedmont lobes (KELLER 1988), *) Adress of the Author: D. Florineth, Geologisches In­ (b) the stratigraphic correlation of the different stitut, Universität Bern, Baltzerstrasse 1, CH-3012 Bern, Switzerland. advances (PENCK & BRÜCKNER 1909; HANTKE 1980; 24 I )( Hl FlORINETH Swiss kilometric grid 19S rivers, lakes X passes Fig. 1: Index map of southeastern Switzerland (Graubünden), northeastern Italy and western Austria with the locations mentioned in the text. Dashed lines give positions of cross - sections (Figs. 4 a and 4b). Abb. 1: Geographische Übersichtskarte der Südostschweiz und der angrenzenden Gebiete Italiens und Öster­ reichs mit den im Text erwähnten Lokalitäten. Die Profilspuren der Fig. 4A und 4B sind ebenfalls angegeben. SCHLÜCHTER 1991), (c) estimations of paleoglacio- their forelands. Despite some uncertainties logical parameters (BLAITER & HAEBERLI 1984), (d) (Pvhein glacier, [KELLER 19931 southern Switzerland the geological evidence for glacier modelling [BINI 1987; FELBER 19931) these survey maps still (HAEBERLI & SCHLÜCHTER 1987) as well as (e) con­ rank as some of the best reconstructions, particu­ clusions about prevailing paleoclimatic conditi­ larly with respect to the accumulation area. It is ons (HAEBERLI 1991a, 1991b). JÄCKLI (1962, 1970) true that paleoglaciological modelling has experi­ compiled a detailed map of the Last Glacial Maxi­ enced significant progress in recent years, but the mum (LGM) for all of Switzerland mostly from lo­ geometry of former glaciers and ice-sheets ne­ cal investigations. The map published by VAN HU­ vertheless remains uncertain in the area above the SEN (1987) covers the LGM in the Eastern Alps and ELA. As the accuracy of each (paleo)glaciological Surface geometry of the Last Glacial Maximum (LGM) in the southeastern Swiss Alps (Graubünden) and its paleoclimatological significance 25 reconstruction is only as reliable as the geologi- tinental climate with a mean annual precipitation cal/geomorphological input data, the basic pro­ amounting to just some 70 - 90 cm per year, the blem of modelling former ice bodies is given by highest parts of these mountains remain glaciated the limited field evidence (overprinting by youn­ today. ger glacier advances, weathering, burial by snow The bedrock geology of the area, described by and sediments, etc.) in the former accumulation various authors (e.g. SPITZ & DYHRENFURTH 1914; area. Thus, due to the results acquired in the ab­ CORNELIUS 1935; BOSCH 1937; HEIERI.I 1955; TRLIMPY lation area, the geometry of the alpine Ice Age I960; SPILLMANN 1993) is important to the present glaciers was generally assumed to be strongly re­ study because most of the glacial history is infer­ lated to the present river system, i.e. ice-flow red from erosional traces on bedrock. This area being the same as today's rivers. This hypothesis exposes Penninic nappes in the west (Margna- seems to be correct for the ablation area where Sella nappe and Platta nappe) and east (Tasna minor variations in bed topography channelled nappe), overlain by a stack of Austroalpine nap­ the massive valley glaciers and stream flow of the pes (Fig. 2). The latter comprise the Upper Aus­ ice predominated. The assumption, however, ap­ troalpine Silvretta nappe (para- and orthogneis- pears less valid at high altitudes in the central ses, amphibolites) to the north, the S-charl-, Quat- Alps, because mapping of glacial-erosion features tervals and Ortler nappes (Triassic and Jurassic indicate up-valley flow of some Ice Age glaciers, sediments) to the east and the Campo/Languard and ice transfluency over high altitude passes. nappe (gneisses) to the sotitheast as well as the Such features are in disagreement with existing Lower Austroalpine Err- and Bernina nappes reconstructions of the LGM. It is therefore evident (crystalline basement and Mesozoic sediments) to the southwest. that a realistic geometry of the last glacial ice bo­ dy cannot be achieved by applying the conclusi­ ons drawn from investigations in the well-docu­ Mapping results mented Swiss Plateau and Prealpes to the poorly Glacial-erosion features and erratics understood inner alpine area. The aim of this research project is to improve our Fig. 3 shows the main localities of mapped glacial understanding of the altitude and topography of erosional features, including trimlines, striations, the accumulation area during the LGM tising geo­ glacial polish, crescentic fractures and gouges as logical and geomorphological evidence. Special well as roches moutonnees. These features are interest is focused on (a) reconstructing flowlines scattered between the bottoms of the valleys and the trimline, superimposed on glacially-moulded of the ice at the LGM by mapped ice flow patterns, bedrock. Glacial polish was found in only a few (b) modelling the ice surface in the former accu­ sites such as passes where ice-flow was constrict­ mulation area by trimline evidence and (c) the ed. The state of preservation of glacial polish and possibilities to draw paleoclimatic conclusions striae is
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