Facies Architecture of a Falling Sea-Level Strandplain, Doce River Coast, Brazil
- D. J. P. Swift3,
- G. F. Oertel3,
- R. W. Tillman4 and
- J. A. Thorne5
Published Online: 14 APR 2009
Copyright © 1991 The International Association of Sedimentologists
Shelf Sand and Sandstone Bodies: Geometry, Facies and Sequence Stratigraphy
How to Cite
Dominguez, J. M. L. and Wanless, H. R. (1992) Facies Architecture of a Falling Sea-Level Strandplain, Doce River Coast, Brazil, in Shelf Sand and Sandstone Bodies: Geometry, Facies and Sequence Stratigraphy (eds D. J. P. Swift, G. F. Oertel, R. W. Tillman and J. A. Thorne), Blackwell Publishing Ltd., Oxford, UK. doi: 10.1002/9781444303933.ch7
Norfolk, Virginia, USA
Tulsa, Oklahoma, USA
Plano, Texas, USA
- Published Online: 14 APR 2009
- Published Print: 30 JAN 1992
Print ISBN: 9780632032372
Online ISBN: 9781444303933
- regressive shelf and coastal sandstones;
- fades architecture of falling sea-level strandplain, Doce River coast, Brazil;
- geomorphological units of Doce strand plain;
- two-dimensional evolutionary scheme of Doce strandplain;
- sedimentary fill of palaeolagoonal depression formed during submergence phase;
- lagoonal deposits associated with submergence phase II;
- littoral zone deposits;
- Bruun's rule and stratigraphic record of littoral zone sequences
The Doce River strandplain, located on the east coast of Brazil, comprises Holocene and Pleistocene beach-ridge terraces, fluvial, lagoonal, freshwater swamp and mangrove swamp deposits.
The Holocene evolutionary history of this strandplain was controlled by the interaction of sea-level changes, riverine sediment supply and wave reworking. The rise in sea-level that followed the last glacial period drowned the Pleistocene strandplain of the Doce River. A barrier-island–lagoonal system formed as a result of this drowning. After 7 ka, with decreasing rates of sea-level rise, the Doce River began emptying into the palaeolagoon and built an intra-lagoonal delta.
During deposition of the late Holocene portion of the strandplain, sea-level dropped 4–5 m from its maximum at about 5.1 ka. During this drop the shoreline downdrift of the river mouth advanced through a mechanism of coastwise extension of sand spits, generating in this process elongate lagoons that later became low-lying areas separated from each other by beach-ridge sets. From 3.8 to 3.5 ka, sea-level rapidly rose 2–3 m above present. The aforementioned low-lying areas were invaded by the sea and became interconnected bays. The updrift side, which prograded through the successive accretion of beach ridges, remained relatively unaffected during this rise. After 3.5 ka, progradation resumed in association with a drop in sea-level.
Theoretical considerations of the Bruun's rule of translation of the shoreface profile shows that during a rise in sea-level, lower shoreface deposits will be preserved preferentially. Conversely, during a drop, only those sediments deposited in the foreshore/upper shoreface will survive. Testing of this model in the study area did not produce conclusive results, probably because the large volume of riverborne sediments masked the effect of sea-level changes during deposition of the littoral zone sequences.