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A Reconstruction of the Last Glacial Maximum (LGM) Ice-Surface Geometry in the Western Swiss Alps and Contiguous Alpine Regions in Italy and France

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A Reconstruction of the Last Glacial Maximum (LGM) Ice-Surface Geometry in the Western Swiss Alps and Contiguous Alpine Regions in Italy and France 0012-9402/04/010057-19 Eclogae geol. Helv. 97 (2004) 57–75 DOI 10.1007/s00015-004-1109-6 Birkhäuser Verlag, Basel, 2004 A reconstruction of the last glacial maximum (LGM) ice-surface geometry in the western Swiss Alps and contiguous Alpine regions in Italy and France MEREDITH A. KELLY1*,JEAN-FRANÇOIS BUONCRISTIANI2 & CHRISTIAN SCHLÜCHTER1 Key words: Glacial trimline, ice-erosional features, last glacial maximum (LGM), western Swiss Alps, geographic information system (GIS), paleoglaciology ABSTRACT ZUSAMMENFASSUNG A reconstruction of the last glacial maximum (LGM) ice-surface geometry in Die Rekonstruktion der Eisoberflächengeometrie während des Letzten Glazi- the western Swiss Alps and contiguous Alpine regions in Italy and France is alen Maximums (LGM) in den westlichen Schweizer Alpen und in angrenzen- based on detailed field mapping of glacial trimlines, ice-erosional features and den Regionen in Italien und Frankreich basiert auf einer detaillierten Kartie- periglacial forms. Field data provide evidence of LGM ice-surface elevations rung von Gletscherschliffgrenzen, Eiserosionserscheinungen und periglazialen and ice-flow directions. The LGM ice surface is portrayed as a grid-format Formen. Diese Geländedaten geben Hinweise auf die Höhe der Eisoberfläche digital elevation model (DEM) using geographic information system (GIS) und die Eisflussrichtungen. Die Eisoberfläche wird durch ein gitterbasiertes software. LGM ice-surface areas and ice volumes in selected regions are calcu- digitales Höhenmodel (DHM) unter Benutzung eines Geographischen Infor- lated using a DEM of the present land topography. The reconstruction de- mations Systems (GIS) dargestellt. Die Eisoberflächenerstreckung und die scribed in this paper is presented in conjunction with a previously determined Eismächtigkeiten werden auf Basis des DHM der gegenwärtigen Landestopo- LGM ice-surface reconstruction for the central and eastern Swiss Alps. graphie berechnet. Die in dieser Veröffentlichung beschriebene Rekonstruk- The LGM ice cap in the western Swiss Alps and contiguous Alpine re- tion wird mit früheren Eisoberflächenrekonstruktionen für das LGM der zen- gions in Italy and France was characterized by transection glaciers. Four main tralen und östlichen Schweizer Alpen verglichen. centers of ice accumulation that influenced the transection glaciers include the Die Eiskappe während des LGM in den westlichen Schweizer Alpen und Rhône ice dome, the Aletsch icefield, the southern Valais icefield, and the Mt. in angrenzenden Regionen in Italien und Frankreich war durch ein Eisstrom- Blanc region. Major ice diffluences were located north of Simplon Pass, on netz charakterisiert. Die vier Zentren der Eisakkumulation, welche das Eis- Gd. St. Bernard Pass and north of present-day Glacier d’Argentière. Estimates stromnetz beeinflussten, waren der Rhône Eisdom, das Aletsch Eisfeld, das of LGM ice volumes in selected regions show that the largest input of ice into Eisfeld im südlichen Wallis und die Mont Blanc Region. Drei Hauptdiffluen- the Rhône Valley was from the southern Valais icefield. Centered in the zen des Eises lagen nördlich des Simplon Passes, auf dem Gd. St. Bernard Pass southern Mattertal, the LGM southern Valais icefield had a surface elevation and nördlich des heutigen Glacier d´Argentière. Die Abschätzung der Eis- of at least 3010 m and an ice thickness of at least 1400 m. The LGM ice-surface mächtigkeit zeigt dass der größte Eintrag von Eis in das Rhônetal vom Eisfeld reconstruction and calculated ice volumes for selected regions are the basis im südlichen Wallis stammte. Mit einem Mittelpunkt im südlichen Mattertal for a hypothesis as to how erratic boulders from the southern Valais and Mt. lag die Oberfläche dieses Eisfeldes in einer Höhe von mindestens 3010 m und Blanc regions were transported to the northern Alpine foreland. Certain LGM hatte eine Eismächtigkeit von mindestens 1400 m. Die Rekonstruktion der centers of ice accumulation and ice-flow directions presented in this paper are Eisoberfläche und die berechneten Eismächtigkeiten sind die Grundlage für also examined for possible paleo-atmospheric circulation information. eine Hypothese, mit welcher der Transport von erratischen Blöcken aus dem Südwallis und der Mont Blanc Region in das Alpenvorland erklärt wird. Die verschiedenen Zentren der Eisakkumulation und die Eisströmungsrichtungen werden zudem in Bezug auf die darin enthaltene Information bezüglich der atmosphärischen Zirkulation während des LGM betrachtet. Introduction The former extents of Swiss Alpine glaciers have been investi- those by de Charpentier (1841), Favre (1884), Penck & Brück- gated for nearly 200 years, since the founding of ancient glacial ner (1909), Frei (1912) and Beck (1926). The most widely cited studies by Jean Pierre Perraudin, Ignace Venetz (1822, 1829) detailed reconstruction of the last maximum ice cap in Switzer- and Louis Agassiz (1837). Early portrayals of a large ice cap in land is based on a compilation of local studies of moraines and the Alps, which extended onto the Alpine forelands, include erosional features published by Jäckli (1962, 1970) (Fig. 1). Re- 1 Institute of Geological Sciences, University of Bern, Baltzerstrasse 1, CH–3011 Bern, Switzerland 2 Université de Bourgogne, UMR 5561 Biogéosciences (équipe D), 6 bd Gabrie, F–21000 Dijon, France *Present address: Byrd Polar Research Center, The Ohio State University, 1090 Carmack Road, Scott Hall 108, Columbus, OH 43210-1002, USA. Email: [email protected]. LMG ice-surface reconstruction, western Swiss Alps 57 LEGEND: 0 115 kilometers Border of Switzerland LGM ice extent on Alpine Foreland Border of the Alps Border of ice-surface reconstruction City Zuerich Wangen a.A. Bern Lat 46o20’N Martigny Fig. 1. Location diagram showing the extent of glaciation on the Alpine forelands during the LGM (after Jäckli 1970). Also shown is the bor- o Long 8 00’E der of the ice-surface reconstruction. search by van Husen (1987), de Beaulieu et al. (1991) and the regions south of the Rhône Valley (Figs. 1, 2). Research Campy & Arn (1991) extend the ice cap reconstruction into was also conducted in Valpelline, Val Veny and Val Ferret, the eastern and southwestern Alps, respectively. Italy, and on the northern side of Mt. Blanc in France. Most studies portray the last maximum ice cap in the inner- Alpine region as an “ice-stream network” and, on the northern Regional geography and southern Alpine forelands, as large piedmont glaciers (Jäckli 1962; Haeberli & Penz 1985). However, a recent de- The upper Rhône Valley dissects the western Swiss Alps, gen- tailed reconstruction shows that the former accumulation zone erally trending to the southwest (Fig. 2). Its headwaters are the in the central and eastern Swiss Alps was not a simple network Rhône Glacier, near Gletsch. In Martigny, the Rhône River of valley glaciers, which generally followed the pre-existing bends to the north-northwest and flows approximately 40 km land topography, but instead was characterized by ice domes to drain into Lake Geneva. North of the Rhône Valley, moun- (Florineth 1998). Three ice domes, or centers of ice accumula- tain peaks in the Aletsch Glacier region, such as Jungfrau, tion, existed in the central and eastern Swiss Alps (Florineth & Mönch and Eiger, are as high as 4000 m. The Aletsch Glacier Schlüchter 1998). Ice flowed outward from the domes in a ra- is about 24 km long and its meltwater outflow, the Massa dial pattern, independent of the pre-existing valley system. The River, enters the Rhône Valley at Brig. South of the Rhône locations of the ice domes are interpreted to reflect areas of Valley, the Valaisian Alps comprise the highest topography in high precipitation and are related to paleo-atmospheric circu- Switzerland. Mountains such as Monte Rosa (4634 m), Mat- lation patterns (Florineth & Schlüchter 1998, 2000). terhorn, (4478 m), and Grand Combin (4314 m) mark the geo- As a continuation of the mapping in the central and eastern graphic border between Switzerland and Italy. Long north- Swiss Alps, we present an ice-surface reconstruction of the last trending valleys, such as Saastal and Mattertal, dissect the high maximum ice cap for the inner-Alpine region of western Valaisian Alps and drain into the Rhône Valley. Two major Switzerland and for contiguous Alpine regions in Italy and alpine passes, Simplon and Gd. St. Bernard, are north-south France (hereinafter referred to as the western Alps). The ice- openings through the Valaisian Alps from Switzerland to Italy. surface reconstruction is based on detailed field mapping of Located on the border of France and Italy, Mt. Blanc (4807 glacial erosional features and digital map analysis using geo- m) is the highest mountain peak in the Alps (Fig. 2). The Mt. graphic information system (GIS) software. Blanc region encompasses numerous high mountains, such as Aiguille d’Argentière (3901 m) and Mt. Dolent (3820 m). Out- let glaciers including Mer de Glace and Glacier d’Argentière Study area exit the Mt. Blanc region to the north. With its headwaters at Within Switzerland, mapping of glacial erosional features was Glacier du Tour, the Arve River drains the Mt. Blanc region to concentrated in Canton Valais west of Fiesch, in particular in the northwest, joining the Rhône River in Geneva. The Mt. 58 M.A. Kelly, J.-F. Buoncristiani & C. Schlüchter LEGEND: Selected present-day glacier 0 35 kilometers * City/Village LGM Trimline Pass LGM ice flow Furka River Border of ice-surface reconstruction Eiger Grimsel Monch Lake International
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