Turbidites and turbidity currents

Tinterri, Roberto; Civa, Andrea; Laporta, Michele; Piazza, Alberto

doi:10.1016/b978-0-444-64134-2.00016-x

Cited by 11 publications

(12 citation statements)

References 117 publications

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“…The logged deposits were described and classified as sedimentary facies, linked to distinctive depositional processes. Most of the facies identified in this study show similarities with the facies described in other deep-water depositional systems (e.g., Pickering and Hiscott, 2015;Tinterri et al, 2020). Further vertical and spatial analysis of the sedimentary logs allowed the recognition of assemblages of related sedimentary facies (facies associations), which were interpreted as representatives of well-established architectural elements (depositional sub-environments) of the deep-water sedimentary system (e.g., Mulder, 2011;Pickering and Hiscott, 2015).…”

Section: Methodssupporting

confidence: 76%

“…Fisher, 1983;Haughton et al, 2003Haughton et al, , 2009Fonnesu et al, 2016). The processes of flow deceleraion, favoured by the tectonically controlled morphologic controls, also may have played an important role in the flow transformation (Tinterri et al, 2016(Tinterri et al, , 2020. In some cases, facies F4 occurs directly above facies F1 and therefore it is considered to have been part of a hybrid event bed (HEB) and corresponds to division H3 of Haughton et al (2009), whereas the sandstones of facies F2 and F3 at the top correspond to division H4.…”

Section: Facies F4: Structureless Muddy Sandstone and Clast-rich Sand...mentioning

confidence: 99%

“…16). This transverse tectonic obstacle could have separated the western and eastern parts of the basin and forced the propagation of sediment gravity flows to the NW (Tinterri et al, 2020(Tinterri et al, , 2022. The confinement also could account for the lack of a clear compensational stacking pattern and a strong aggradation trend of the depositional lobe in the Lubinka section (Fig.…”

Section: Stage 1 (S1): Early Campanianmentioning

confidence: 99%

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Evolution of a turbidite system in a narrow basin setting: the Ropianka Fm (Campanian–Paleocene) in the Skole Nappe of the Polish Carpathians

Łapcik

2024

ASGP

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Facies analysis plays an important role in basin analysis and serves as a tool to track the evolution of fossil depositional environments. This also applies to the deep-water setting, where turbidite systems represent an ultimate sink for the vast majority of sedimentary materials on Earth, including anthropogenic pollutants (e.g., Martin et al., 2022). The consequence of the capturing and burial of these deposits has also a great influence on carbon sequestration and climate (e.g., Arthur et al., 1988). Our understanding of the architecture and evolution of deep-water systems is constantly growing and models for facies prediction are now better than ever. However, the multiplicity of factors, which strongly influence turbidite systems (e.g., nature of the source, tectonic setting, eustatic sea-level changes, climate), leads to a wide variety of ancient records and proposed models that describe them (e.g.

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Section: Methodssupporting

confidence: 76%

Section: Facies F4: Structureless Muddy Sandstone and Clast-rich Sand...mentioning

confidence: 99%

Section: Stage 1 (S1): Early Campanianmentioning

confidence: 99%

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Evolution of a turbidite system in a narrow basin setting: the Ropianka Fm (Campanian–Paleocene) in the Skole Nappe of the Polish Carpathians

Łapcik

2024

ASGP

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“…These sandstones are interpreted as having been deposited layer‐by‐layer from non‐cohesive, partly to fully turbulent, low to high‐density turbidity currents (e.g. Lowe, 1982; Postma, 1986; Mulder & Alexander, 2001; Mutti et al ., 2009; Talling et al ., 2012; Tinterri et al ., 2020). Normal grading, planar bedding and traction structures point to deposition from fully turbulent, low‐density turbidity currents.…”

Section: Resultsmentioning

confidence: 99%

Gravitational resedimentation as a fundamental process in filling fjords: Lessons from outcrops from a late Palaeozoic fjord in Namibia

Menozzo da Rosa,

Isbell,

McNall

et al. 2023

Sedimentology

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The stratigraphic architecture of fjords is complicated due to the delicate interplay between ice dynamics, sediment supply, relative sea‐level fluctuations and slope failures. Glaciogenic sediment is prone to failure and to be carried downslope to the fjord floor through the entire spectrum of mass movements and subaqueous density flows, as the unstable paraglacial submarine landscape moves toward stability. Palaeofjords formed by Gondwanan glaciers during the late Palaeozoic Ice Age contain a compelling record of gravitational resedimentation in fjord depositional systems. This paper showcases the geomorphology and depositional history of a glacial cycle in the Orutanda fjord in north‐western Namibia as an example of an overdeepened fjord basin fill dominated by products of subaqueous gravitational processes. During glaciation, the Orutanda glacier carved a 20 km long by 3.7 km wide glacial trough that embodies an overdeepened basin. Ice thickness during terminal glacial occupation of the fjord is estimated to had been up to 200 m based on the fjord geomorphology. The progressive retreat of the tidewater glacier, concomitant with marine flooding, increased accommodation space in the overdeepened basin during deglaciation. During this stage, proglacial sedimentation through iceberg rafting and settling of turbid plumes was outpaced by intense paraglacial downslope resedimentation of glacially‐transported debris. Successive failures from the fjord walls and downslope resedimentation resulted in coalescing debrite–turbidite lobes on the fjord floor. Slide deposits, composed entirely of deformed debrites and turbidites, indicate these resedimented facies were prone to renewed mass wasting. As the Orutanda glacier melted, the fjord experienced the axial progradation of a fjord‐head delta registered only by turbidites and slide deposits derived from its collapse. The Orutanda fjord sheds light on the relevance of paraglacial mass wasting in overprinting glaciogenic deposits. This insight is key to understanding the role of glaciers versus non‐glacial processes in producing the glacial deep‐time record.

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“…The former, consisting of very fine-grained sandy siltstone rich in load structures without mudstone clasts, is associated with deceleration and reflection of low-density turbidity currents in basin plains against distal morphological obstacles. On the contrary, the latter consists of muddy sandstone rich in mudstone clasts and soft-sediment deformation produced by decelerations, induced by a gradient decrease, of mud-rich turbidity currents, whose mud enrichment must occur upcurrent, generally induced by a tectonic confinement that favor erosive processes (Tinterri et al, 2020; see Figure 12).…”

Section: Formation and Significance Of Slurry Facies In Contained And...mentioning

confidence: 99%

Contained-Reflected Megaturbidites of the Marnoso-arenacea Formation (Contessa Key Bed) and Helminthoid Flysches (Northern Apennines, Italy) and Hecho Group (South-Western Pyrenees)

2022

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Contained-reflected beds deposited by fully-ponded or partially-reflected turbidity currents are important because their correct evaluation can give important indications on the degree of basin confinement and on the type, size and orientation of the morphological obstacle. Through a detailed facies analysis of various significant megabeds in the Marnoso-arenacea Formation, including the Contessa key bed, in the helminthoid flysches in the northern Apennines (Italy) and in the Pyrenees (megaturbidite MT5), this work proposes a depositional model that is well consistent with the recent experimental data available in the literature, discussing their strengths and limits. The Contessa and flysch megabeds fit very well with the experimental conditions because they are deposited in narrow and elongated confined basins characterized by axial flows. Indeed, in the proposed model, it is possible to recognize facies deposited by: 1) a basal underflow directed towards the bounding slope (Facies A), 2) an intermediate part of the flow characterized by lateral deflections (facies B1), 3) an upper well-developed reversing flow (facies B2) and 4) an uppermost residual reversing flow recording the final collapse of the fine-grained suspended load forming a poorly-sorted slurry facies C and a very thick mudstone unit D. Facies A, B1 and B2 are usually separated by very thin fine-grained muddy drapes rich in carbonaceous matter, which can be traced throughout the basin. These drapes - very common in contained and confined beds in these settings - can be related to internal density surfaces, along which decoupling processes, separating underflows from reversing overflows, can easily occur. Conversely, as the MT5 is characterized by a source transversal to an elongated narrow basin, the large flow volume versus basin capacity hinders the generation of reversing flows and rebound layers favoring the formation of fully-ponded pulsating overflows able to deposit alternations of laminated and massive units. This facies type can be observed in the basins that are characterized by axial flows only near the basin margins where the pulsating collapse of the reversing flow can dominate. This study shows that the integration of detailed field studies are essential to validate experimental data from an applicative point of view.

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Turbidites and turbidity currents

Cited by 11 publications

References 117 publications

Evolution of a turbidite system in a narrow basin setting: the Ropianka Fm (Campanian–Paleocene) in the Skole Nappe of the Polish Carpathians

Evolution of a turbidite system in a narrow basin setting: the Ropianka Fm (Campanian–Paleocene) in the Skole Nappe of the Polish Carpathians

Gravitational resedimentation as a fundamental process in filling fjords: Lessons from outcrops from a late Palaeozoic fjord in Namibia

Contained-Reflected Megaturbidites of the Marnoso-arenacea Formation (Contessa Key Bed) and Helminthoid Flysches (Northern Apennines, Italy) and Hecho Group (South-Western Pyrenees)

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