Land–sea correlation between Late Holocene coastal and infralittoral deposits in the SE Iberian Peninsula (Western Mediterranean)

Fernández-Salas, L.M.; Dabrio, Cristino J.; Goy, José Luis Goy; Río, Víctor Díaz del; Cardeña, Caridad Zazo; Lobo, F. J.; Sanz, J. L.; Lario, Javier

doi:10.1016/j.geomorph.2008.05.013

Cited by 45 publications

(40 citation statements)

References 9 publications

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“…In contrast, the elongated plan-view geometries typical of delta-scale subaqueous clinoforms strike parallel to the alongshore advective transport belt that feeds and sculpts them (Fig. 4;Field and Roy, 1984;Driscoll and Karner, 1999;Hernández-Molina et al, 2000a;Cattaneo et al, 2003Cattaneo et al, , 2007Liu et al, 2007;Fernández-Salas et al, 2009;Mitchell et al, 2012;. As shown schematically in Fig.…”

Section: Controls On the Evolution Of Delta-scale Subaqueous Clinoformsmentioning

confidence: 99%

Quantitative characterisation of deltaic and subaqueous clinoforms

Patruno

Hampson

Jackson

2015

Earth-Science Reviews

215

272

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Clinoforms are ubiquitous deltaic, shallow-marine and continental-margin depositional morphologies, occurring over a range of spatial scales (1-10 4 m in height). Up to four types of progressively larger-scale clinoforms may prograde synchronously along shoreline-to-abyssal plain transects, albeit at very different rates. Paired subaerial and subaqueous delta clinoforms (or 'delta-scale compound clinoforms'), in particular, constitute a hitherto overlooked depositional model for ancient shallow-marine sandbodies. The topset-to-foreset rollovers of subaqueous deltas are developed at up to 60 m water depths, such that ancient delta-scale clinoforms should not be assumed to record the position of ancient shorelines, even if they are sandstone-rich. This study analyses a large dataset of modern and ancient delta-scale, shelf-prism-and continental-margin-scale clinoforms, in order to characterise diagnostic features of different clinoform systems, and particularly of deltascale subaqueous clinoforms. Such diagnostic criteria allow different clinoform types and their dominant grain-size characteristics to be interpreted in seismic reflection and/or sedimentological data, and prove that all clinoforms are subject to similar physical laws. The examined dataset demonstrates that progressively larger scale clinoforms are deposited in increasingly deeper waters, over progressively larger time spans. Consequently, depositional flux, sedimentation and progradation rates of continental-margin clinoforms are up to 4-6 orders of magnitude lower than those of deltas. For all clinoform types, due to strong statistical correlations between these parameters, it is now possible to calculate clinoform paleobathymetries once clinoform heights, age spans or progradation rates have been constrained. Muddy and sandy delta-scale subaqueous clinoforms show many different features, but all share four characteristics.(1) They are formed during relative sea-level stillstands (e.g., Late Holocene); (2) their stratigraphic architecture and facies character are dominated by basinal processes, and are quite uniform; (3) their plan-view morphology is shore-parallel and laterally extensive; (4) their sigmoidal cross-sectional geometry contrasts with the oblique profiles of most subaerial deltas. Holocene-age, delta-scale, sand-prone subaqueous clinoforms occur on steep (≥0.26°) and narrow (5-32 km) shelves, at typical distances of 0.6-7.2 km from the shoreline break. That contrasts with mud-prone subaqueous deltas, which form clinoforms on gently-sloping (0.01-0.38°), wide (23-376 km) shelves, at usual distances of 7.5-125 km from the shoreline. Delta-scale sand-prone subaqueous clinoforms have diagnostically steep foresets (0.7-23°). Similarly steep gradients were observed in much larger shelf-prism-and continental-margin-scale clinoforms. Gentler foreset gradients are shown by sand-prone subaerial deltas (0.1-2.7°), and mud-prone subaqueous and subaerial deltas (0.03-1.50°). Due to the lack of connections with river mouths, Holocene delta-scale sa...

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Section: Controls On the Evolution Of Delta-scale Subaqueous Clinoformsmentioning

confidence: 99%

Quantitative characterisation of deltaic and subaqueous clinoforms

Patruno

Hampson

Jackson

2015

Earth-Science Reviews

215

272

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“…Recent sand-prone delta-scale subaqueous clinoforms, on the contrary, form actively-accreting shore-parallel clastic wedges on narrow (< 35 km) and steep (≥0.26°) high-energy shelves, between fairweather and storm wave bases, and are commonly associated with nondeltaic shorelines and strandplains (Fernández-Salas et al, 2009;Patruno et al, 2015a). Examples include the clinoforms offshore Australia and New Zealand (Field and Roy, 1984;Dunbar and Barrett, 2005); southern Spain-Portugal (Hernández-Molina et al, 2000a;Lobo et al, 2005;Fernández-Salas et al, 2009) (Fig.…”

Section: Delta Scale Clinoformsmentioning

confidence: 99%

“…Examples include the clinoforms offshore Australia and New Zealand (Field and Roy, 1984;Dunbar and Barrett, 2005); southern Spain-Portugal (Hernández-Molina et al, 2000a;Lobo et al, 2005;Fernández-Salas et al, 2009) (Fig. 13c), and California (Chin et al, 1988;Le Dantec et al, 2010).…”

Section: Delta Scale Clinoformsmentioning

confidence: 99%

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

Patruno

Helland‐Hansen

2018

Earth-Science Reviews

187

166

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A B S T R A C TClinoforms are inclined and normally basinward-dipping horizons developed over a range of spatial and temporal scales in both siliciclastic and carbonatic systems. The study of clinoform successions underpins sequence stratigraphy and all efforts to reconstruct the relative partitioning of reservoir, seal and source rocks along shoreline to basin-floor profiles.Here, we review clinoform research and propose a more systematic description and classification of clinoforms. This is a crucial step to improve predictions of facies and lithology distribution within shoreline to continental shelf and abyssal plain successions, together with the genesis, drivers and dynamics of their constituent sedimentary units.Four basic clinoform types are here distinguished in delta/shorelines, lacustrines and marine environments, on the basis of their overall spatial and temporal scale, morphology, outbuilding dynamic and geodynamic and depositional setting: (1, 2) delta-scale clinoforms, which in turns are sub-divided into shoreline and delta-scale subaqueous clinoforms; (3) shelf-edge clinoforms; and (4) continental-margin clinoforms. Delta-scale clinoform sets are tens of metres high and typically represent 1-10 3 kyr, with progradation rates ranging from 1,000-100,000 m/kyr for shorelines and "subaerial deltas" to 100-20,000 m/kyr for subaqueous deltas; shelfedge clinoform sets are hundreds of metres high and are nucleated and accreted in 0.1-20 Myr (usual progradation rates of 1-100 m/kyr) by successive cross-shelf transits of delta-scale clinoforms; continental-margin clinoform sets are thousands of metres high, hallmark key geodynamic/crustal boundaries (e.g., continent/ocean transition) and slowly prograde basinwards in ca. 5-100 Myr, with typical rates of 0.1-10 m/kyr. As a consequence of the very different progradation rates and of the difficulty of large-scale clinothems to backstep during transgressions, shorelines are the most dynamic clinoforms with regards to position, continental margins the least, and shelf-edges are intermediate. Shortly after a transgression, therefore, the four clinoform types may prograde synchronously along shoreline-to-abyssal plain transects, forming "compound clinoform" systems. During the subsequent regressive cycle, however, due to the dissimilarity in progradation rates, different clinoform types will normally merge progressively with each other, giving rise to "hybrid clinoforms" (e.g., shelf-edge deltas), and fewer depositional breaks-in-slope are distinguished along a single shoreline-toabyssal plain transect. Overall, all clinoform systems are the result of the dynamic evolution of compound and hybrid clinoforms along a temporal and spatial continuum, regulated by the cyclical backstepping of the smallerscale system within natural progradational-retrogradational cycles of larger-scale clinothem outbuilding.All clinothem types may show either an accretionary/active or draping/passive style, depending on the proximity to the sediment source. Draping clinothems are nearly...

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“…11). Tais prismas, no entanto, são interpretados no presente estudo como depósitos do conjunto de feições que compõem o ambiente infralitorâneo, característico de plataformas internas dominadas por ondas (Hernández-Molina et al, 2000b), inclusive quando presentes componentes de transporte lateralà costa (longshore currents , Fernández-Salas et al, 2009). Seriam, deste modo, corpos sedimentares que progradam de forma submersa, paralelamenteà costa, como parte integrante do Trato de Sistema de Mar Alto , e cuja ruptura de gradiente (frente inclinada de progradação) corresponderia ao nível médio de base em regime de ondas de tempestade (Hernández-Molina et al, 2000b;Fernández-Salas et al, 2009).…”

Section: Comparação Da Interpretação Das Feições Morfológicas Propostunclassified

“…Tais prismas, no entanto, são interpretados no presente estudo como depósitos do conjunto de feições que compõem o ambiente infralitorâneo, característico de plataformas internas dominadas por ondas (Hernández-Molina et al, 2000b), inclusive quando presentes componentes de transporte lateralà costa (longshore currents , Fernández-Salas et al, 2009). Seriam, deste modo, corpos sedimentares que progradam de forma submersa, paralelamenteà costa, como parte integrante do Trato de Sistema de Mar Alto , e cuja ruptura de gradiente (frente inclinada de progradação) corresponderia ao nível médio de base em regime de ondas de tempestade (Hernández-Molina et al, 2000b;Fernández-Salas et al, 2009). Desta forma, no presente estudo os traços morfológicos expressos ao longo das isóbatas de 50 e 100 m são atribuídos a feições morfossedimentares do ambiente progradacional costeiro representati- vas, provavelmente, das fácies distais menos arenosas desenvolvidas durante, respectivamente, os Tratos de Sistema de Mar Alto das sequências Sq5 (Holoceno ainda em construção) e Sq4 (subestágios isotópicos marinhos 5e, 5c e 5a e o estágio isotópico 3 durante o Pleistoceno Superior, Fig.…”

Section: Comparação Da Interpretação Das Feições Morfológicas Propostunclassified

Feições geomorfológicas indicativas de variações eustáticas e de exposição subaérea da plataforma continental sul fluminense durante o pleistoceno superior-holoceno*

Reis¹,

Maia²,

Silva³

et al. 2011

Rev. Bras. Geof.

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ABSTRACT. The analysis of sparker monochannel seismic lines, coupled with a stratigraphic framework recently proposed for the study area, allowed us to put forward a new glacio-eustatic scenario and to reinterpret the origin of several seafloor features located along the 50, 100, 110, 130 and 150 m isobaths. Our seismic stratigraphic and geomorphological analyses revealed that a wide variety of depositional processes were involved in the formation of these features. Sea-floor features observed near 50 and 100 m water depths, previously interpreted as paleo-coastlines developed at periods of stillstand in the course of the Holocene Transgression, are reinterpreted as the inclined frontal clinoforms of prograding sedimentary prisms deposited during the maximum highstands from, respectively, the Holocene and the Late Pleistocene (marine isotopic substages 5e, 5c and 5a and isotopic stage 3). Also, the escarpments and associated basal flat surfaces located around the 130 and 110 m isobaths, previously interpreted as nearshore systems developed close to the glacial maximum and during stillstands of the last deglaciation, respectively ∼15 ky B.P. and ∼13 ky B.P., are reinterpreted, together with a scarp found near the 150 m isobaths, as erosional remnants sculpted under forced regressive conditions during the Wisconsin Regression and preserved as a succession of flat surfaces that become gradually deeper and younger towards the shelf break.Keywords: continental shelf, marine geomorphology, forced regression, late Pleistocene, Holocene deposits. RESUMO.A interpretação de perfis de sísmica de reflexão monocanal sparker, integrada ao arcabouço estratigráfico recentemente proposto para a plataforma continental fluminense, permitiu uma nova interpretação em outros contextos de oscilações glacioeustáticas para a formação das feições de fundo anteriormente reconhecidas ao longo das isóbatas de 50 m, 100 m, 110 m, 130 m e 150 m. As feições ao longo das isóbatas de 50 m e 100 m, anteriormente interpretadas como paleolinhas de costa desenvolvidas em posições de nível de mar estacionário durante a Transgressão Holocênica, foram reinterpretadas como faces frontais inclinadas de prismas sedimentares progradantes de nível de mar alto, respectivamente do Holoceno e do Pleistoceno Superior (subestágios isotópicos marinhos 5e, 5c e 5a e o estágio isotópico marinho 3). As escarpas e os patamares erosivos ao longo das isóbatas de 110 m e 130 m foram antes interpretados como sistemas costeiros praiais esculpidos durante o máximo glacial (escarpa a -130 m, a ∼15 ka) e durante níveis de mar estacionários daúltima deglaciação (escarpa a -110 m, a ∼13 ka). Neste trabalho estas feições, juntamente com o escarpamento a -150 m, foram reinterpretados como remanescentes erosivos formados em condições de regressão forçada em períodos de aceleração de queda ou de estabilização de nível eustático durante a Regressão Wisconsiniana, hoje preservados como feições sucessivamente mais profundas e jovens em direçãò a borda de plataforma.Palavras-chave: pl...

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Land–sea correlation between Late Holocene coastal and infralittoral deposits in the SE Iberian Peninsula (Western Mediterranean)

Cited by 45 publications

References 9 publications

Quantitative characterisation of deltaic and subaqueous clinoforms

Quantitative characterisation of deltaic and subaqueous clinoforms

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

Feições geomorfológicas indicativas de variações eustáticas e de exposição subaérea da plataforma continental sul fluminense durante o pleistoceno superior-holoceno*

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