Abstract
The upper part of the Lower Miocene Sloboda Conglomerate, a 250–1400 m thick unit, was deposited mainly on an alluvial fan and fan delta during the early stages of Carpathian Foredeep development. During of the Old Styrian overthrust movements of the Carpathian orogen, a forebulge was formed, which supplied clasts to the conglomerate. The clasts are dominated by Late Proterozoic–Early Cambrian phyllites, while Paleozoic carbonates are common, and Mesozoic and other rocks are rare. The source area formed mainly by a prolongation of the Małopolska Massif that was involved in the forebulge; this was located close to a palaeovalley cut into Mesozoic and Paleozoic rocks, buried under younger strata. Additional material was derived from the advancing front of the Carpathian Flysch nappes.  
Highlights
INTRODUCTIONDuring the transition from a remnant oceanic to a peripheral foreland basin, shallow-marine and continental molasse sediments accumulate, both on top of an accretionary wedge (piggyback basin) as well on top of a pre-existing foreland platform basement (foredeep basin, see Einsele, 2000)
During the transition from a remnant oceanic to a peripheral foreland basin, shallow-marine and continental molasse sediments accumulate, both on top of an accretionary wedge as well on top of a pre-existing foreland platform basement
Conglomerate, a 250–1400 m thick unit that is known from surface exposures of the Boryslav–Pokuttya Nappe and the subsurface succession of the Sambir (Stebnyk) Nappe across a limited area of the Eastern Carpathians (Fig. 1)
Summary
During the transition from a remnant oceanic to a peripheral foreland basin, shallow-marine and continental molasse sediments accumulate, both on top of an accretionary wedge (piggyback basin) as well on top of a pre-existing foreland platform basement (foredeep basin, see Einsele, 2000). A – conglomerates alternating with sandstone beds; the sandstone bed from the right is wedge-shaped; B – sandstones (to the left) covered by conglomerates of fluctuating clast size and matrix content; C – conglomerate-sandstone beds, mudstones in the upper part; the middle sandstone bed is cross-bedded; inclination of laminae points to transport to the north-east (red arrow); D – cross-bedded sandstones, siltstones and mudstones and a lens of fine-grained conglomerate (cgl); inclination of laminae points to transport to the north-east (red arrow); in A and B, bedding subvertical, top from the right poorly sorted, clast-supported, cobble-boulder conglomerates can be interpreted as debris flows (DeCells et al, 1991), including pebble-cobble conglomerates which are inversely-to-normal and inversely graded, with larger clasts “floating” at the tops of beds (Rohais et al, 2008) Such a mechanism can explain the general absence of scouring and channelling. This corresponds well to the early stage of subsidence in the Carpathian Foredeep caused by nappe loading (Kováč et al, 1998; Oszczypko, 1998; Oszczypko et al, 2006)
Sign-in/Register to view highlights & summary 
Published Version (
Free)
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 call