Abstract
Abstract. A thrust-bound footwall syncline located within the proximal part of the southern Jasmund Glacitectonic Complex is investigated, exploring the spatio-temporal relationship between glacitectonic macro- and microstructures. Orientation and geometry of macroscale folds and thrust faults reveal a two-phased deformation history recorded by the sedimentary sequence. The deformation is a result of glacitectonic imbrication and subsequent ice flow across Jasmund Peninsula during the late Weichselian. Clast microfabrics preserved within the folded glacial diamicts reveal that till-internal deformation is mainly related to subglacial shearing within the glacier bed, which predates large-scale imbrication and folding.
Highlights
The syncline of Pleistocene Stripe 4 (Streifen 4) is located at a coastal cliff section northeast of Lenzer Bach near the town Sassnitz (54◦31 42.24 N, 13◦40 25.99 E)
Chitectural geometries, recognition of crosscutting relationships between the depositional units and identification of glacitectonic structures, an imbricate thrust-stack model was eventually developed for the glacitectonic evolution of the Jasmund Peninsula during the Weichselian glaciation (e.g. Steinich, 1972; Groth, 2003; Ludwig, 2011)
The analysis of microstructures observed in thin sections obtained from glacial diamicts on Jasmund revealed a relative chronology of deformational events, which can be interpreted in the context of syn-depositional till-forming processes and subsequent post-depositional modification (Brumme, 2015; Brumme et al, 2019)
Summary
The syncline of Pleistocene Stripe 4 (Streifen 4) is located at a coastal cliff section northeast of Lenzer Bach near the town Sassnitz (54◦31 42.24 N, 13◦40 25.99 E). Chitectural geometries, recognition of crosscutting relationships between the depositional units and identification of glacitectonic structures, an imbricate thrust-stack model was eventually developed for the glacitectonic evolution of the Jasmund Peninsula during the Weichselian glaciation In early 2012, a cliff failure formed a new exposure that exhibited the fold in modified geometry and detail including a metre-scale second-order parasitic fold at the centre of the syncline and a drag fold at its southern limb (Fig. 1). These circumstances allowed for a new in-depth macro- and microstructural investigation (Mehlhorn, 2016). Note that all measurements of planes indicate direction and inclination of the dip
Sign-in/Register to view highlights & summary Sign-in/Register to access full text options 
Talk to us
Join us for a 30 min session where you can share your feedback and ask us any queries you have
Schedule a callDisclaimer: All third-party content on this website/platform is and will remain the property of their respective owners and is provided on "as is" basis without any warranties, express or implied. Use of third-party content does not indicate any affiliation, sponsorship with or endorsement by them. Any references to third-party content is to identify the corresponding services and shall be considered fair use under The CopyrightLaw.
