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We combine 10Be surface exposure ages from boulders and bedrock, field observations and measurement of bedrock ice‐flow direction indicators with numerical ice surface models to develop a model of the evolution of the Oberhasli area in the central Swiss Alps from the Last Glacial Maximum (LGM) to the early Holocene. Surface exposure ages from bedrock and boulder samples imply that the highest ice surface at the glacial trimline in Haslital was attained at 23.0 ± 0.8 ka. Significant retreat followed no later than 17.7 ± 0.8 ka. Several boulders were let down on the Gelmerhörner ridge during lowering of the ice surface of the Aare LGM glacier. Their exposure ages of 16–14 ka suggest that patches of remnant ice persisted on the trough shoulder until the Bølling–Allerød interstadial. Lateglacial glacier systems in the High Alps were of a dendritic character, confined to the trunk valleys and cirques. Based on combined evidence from glacial erosional marks, surface exposure ages and numerical modelling we have been able to constrain the likely terminal position and ice surface of the Egesen stadial glacier (Younger Dryas equivalent) in Haslital. Exposure ages from the trough floor imply that deglaciation was completed at the end of the Younger Dryas at 12.2–10.8 ka.

The Tatra Mountains extend along the border between Slovakia and Poland in the Western Carpathians. It is the highest and formerly one of the most glaciated massifs in the entire Carpathian mountain chain. We present a paleoglaciological map of the Tatra Mts. and its foreland (ca. 1270 km 2 ) for the Last Glacial Maximum (LGM) at the scale 1:50 000. We re-evaluate geomorphological evidence for all Tatra glacial systems identified in the literature based on new field mapping and remote sensing data analysis. Utilizing geographic information systems (GIS) and 10 m resolution digital elevation model (DEM) as a base topography, we have reconstructed, for the first time, the detailed extent and surface geometry of all Tatra LGM glaciers (55 glacier systems, total area ca. 280 km 2 ) based on the distribution of glacial erosional and depositional landforms. Our research results confirm stronger glaciation on the southern slopes of the Tatras due to local topography. We also conclude that distinct morainic amphitheaters, which predominate on the southern side of the highest, eastern part of the Tatras, were formed by debris-covered glaciers.

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