Sedimentary Geology 429 (2022) 106077 Contents lists available at ScienceDirect Sedimentary Geology journal homepage: www.elsevier.com/locate/sedgeo Sharp-based, mixed carbonate–siliciclastic shallow-marine deposits (upper Miocene, Betic Cordillera, Spain): The record of ancient transgressive shelf ridges? M. Poyatos-Moré a,b,⁎, F. García-García c, F.J. Rodríguez-Tovar c, J. Soria d, C. Viseras c, F. Pérez-Valera c, I. Midtkandal b a Departament de Geologia, Universitat Autònoma de Barcelona, 08193 Cerdanyola del Vallès, Barcelona, Spain b Department of Geosciences, University of Oslo, Sem Sælands vei 1, 0371 Oslo, Norway c Departamento de Estratigrafía y Paleontología, Universidad de Granada, Avenida de la Fuente Nueva S/N, 18071 Granada, Spain d Departamento de Ciencias de la Tierra y del Medio Ambiente, Universidad de Alicante, 03690 Sant Vicent del Raspeig, Spain a r t i c l e i n f o a b s t r a c t Article history: Isolated sharp-based sedimentary bodies in shelf settings can develop via the reworking of regressive deposits dur- Received 18 October 2021 ing transgressions. An example of these are shelf ridges, formed under a wide range of processes, and widely studied Received in revised form 28 December 2021 due to their high reservoir potential. However, there is still a lack of examples in mixed (carbonate–siliciclastic) suc- Accepted 28 December 2021 cessions. This study presents an outcrop example from the Upper Miocene of the Betic Cordillera (Spain), with the Available online 6 January 2022 aim to propose a model for the development of transgressive sharp-based mixed carbonate–siliciclastic deposits, Editor: Dr. Jasper Knight and to provide criteria to differentiate these from their regressive counterparts. The studied succession is ca. 300 m-thick, and shows a cyclic alternation of coarse and fine-grained mixed deposits. Depositional cycles start with siliciclastic-dominated offshore to offshore transition deposits, progressively replaced by lower shoreface deposits. Keywords: These are abruptly truncated by sharp erosive contacts bioturbated by passively-infilled large burrows; their Mixed carbonate–siliciclastic ichnological features allow assignation to the Glossifungites ichnofacies. These contacts are interpreted as ravinement Shelf ridge surfaces. They are overlain by mixed carbonate–siliciclastic barforms, rich in skeletal fragments and extraclasts, and Transgressive displaying large-scale cross bedding. These form several m-thick and hundreds of m-long depositional elements Ravinement interpreted as mixed shelf ridges. These ridges formed in a fine-grained, shallow-water shelf, which occasionally re- Glossifungites ceived coarse siliciclastic sediment supply via gravity flows, but had a coeval offshore carbonate factory, which pro- vided the skeletal fragments. The sharp-based, coarser-grained nature and lithological break at the base of these mixed carbonate–clastic deposits could lead to their misinterpretation as forced-regressive wedges. However, the nature of their lower contact, combined with the reworked offshore skeletal fragments, and their stacking pattern are consistent with these mixed units forming during transgression. Other studies in relatively time-equivalent de- posits have demonstrated the existence of coeval regressive, coarser siliciclastic-dominated shoreline systems in rel- atively close localities. These evidence a complex basin configuration in the area during the upper Miocene, with the development of local depocentres and relatively narrow corridors or seaways in the Mediterranean–Atlantic con- nection, which could have favoured shelf reworking processes, but also promoted the development of diverse stack- ing patterns, reflecting the differential interaction between active tectonics and sedimentation across the region. © 2022 The Author(s). Published by Elsevier B.V. This is an open access article under the CC BY-NC-ND license (http://creativecommons.org/licenses/by-nc-nd/4.0/). 1. Introduction interpreted them as incised valley fills or regressive shallow-marine de- posits, transported onto and across the shelf during periods of abrupt The origin of sharp-based coarse-grained sedimentary bodies iso- lowering of relative sea level (e.g., Plint, 1988; Van Wagoner, 1991; lated in fine-grained dominated offshore/shelf settings has been a mat- Posamentier and Chamberlain, 1993; Bergman and Walker, 1995, ter of debate for the sedimentary community (see Snedden and 1999; Burton and Walker, 1999; MacEachern et al., 1999). Alternatively, Bergman, 1999; Suter and Clifton, 1999). Some studies originally another mechanism involves the reworking of regressive deposits by shelf processes during transgressions. This can result in the develop- ⁎ Corresponding author at: Departament de Geologia, Universitat Autònoma de ment of shelf ridges, which are relatively large-scale (several m-high, Barcelona, 08193 Cerdanyola del Vallès, Barcelona, Spain. hundreds of m-wide, few km long) elongate geomorphic elements ob- E-mail address: miquel.poyatos@uab.cat (M. Poyatos-Moré). served in a wide range of either tide-, wave- or storm-dominated https://doi.org/10.1016/j.sedgeo.2021.106077 0037-0738/© 2022 The Author(s). Published by Elsevier B.V. This is an open access article under the CC BY-NC-ND license (http://creativecommons.org/licenses/by-nc-nd/4.0/). M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 Guada 500000 UTM 490000 510000 C coordinates Pozo Alcón le 480000 ntín Lirio 4170000 riv er Coto Cherrín Fig. 2 er r riv eno Media Guadiana M Fanega Picacho Alicún La Lancha de Ortega Cuevas del Campo Al ic r ún rive Dehesas de Guadix Tamojares Tetinos 4160000 er riv Forruchu Salinas es Negratín water reservoir Montes Orientales rd Fa Negral Villanueva de las Torres N G 0 2 4 6 8 10 km Pedro or T ri v Martínez T er T Stratigraphic Exorheic (external Age units drainage) units Final-filling surface: pedogenic carbonates Pleistocene Fluvial deposits VI Fluvial lutites, gravels channels and palustrine carbonates Pliocene Endorheic T T T Carbonatic tufa continental units Marginal alluvial fan conglomerates and fluvial lutites with Turolian V gravels channels; basinal lacustrine clays and palustrine carbonates Late Miocene IV Globorotalia menardii gr. Deltaic conglomerates and basinal planktonics rich marls III (sinistral) 7.58 - 7.51 Ma Deltaic conglomerates, shallow marine calcarenites, and coral reefs Globorotalia suterae late II 7.80 Ma Marginal shallow marine calcarenites and basinal planktonics rich marls Tortonian Marine I Studied units interval Planktonics rich marls with mixed siliciclastic-carbonate sandstones Early-Middle Basement Neogloboquadrina Miocene acostaensis (dextral) 9.54 Ma Skeletal, temperate water, carbonates (early Tortonian): Algal Limestones Triassic Median Subbetic: clays, sandstones, carbonates and, locally, volcanic rocks Fig. 1. Location map of the study area within the Iberian Peninsula (A) and in the Betic Cordillera (B), in southern Spain. (C) Geological map (and legend) of the study area, ca. 5 km NE of Alicún de Ortega. Modified from Soria (1993). 2 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 modern (e.g., Houbolt, 1968; Swift, 1975; Kenyon et al., 1981; Swift and calcarenites and conglomerates, and defined by Neogloboquadrina Field, 1981; Stride, 1982; McBride and Moslow, 1991; Johnson and acostaensis to N. humerosa planktonic foraminifera subzones (Soria, Baldwin, 1996; van de Meene et al., 1996; Berné et al., 1998; Snedden 1993); Unit II, dominated by offshore marine marlstones interbedded and Dalrymple, 1999; Dyer and Huntley, 1999; Jin and Chough, 2002; with occasional dm-thick sandstones, and defined by Globorotalia Snedden et al., 2011) and ancient shelves (e.g. Posamentier, 2002; suterae planktonic foraminifera subzone; and Unit III, represented by Olariu et al., 2012; Schwarz, 2012; Messina et al., 2014; Leva-López nearshore cross-stratified mixed siliciclastic–carbonate deposits and et al., 2016; Longhitano et al., 2021). Shelf ridge deposits are commonly large-scale cross-bedded conglomerates (Soria, 1993; Soria et al., well sorted, relatively texturally and mineralogically mature, and with 2003; Reolid et al., 2012). extensive and well-preserved overlying and interstratified fine- The succession crops out in a regional monoclinal structure with grained successions, which give them potential to form good reservoirs strata consistently dipping to the S–SW (Fig. 1). This overall disposition (e.g., Posamentier, 2002; Cattaneo and Steel, 2003; Chiarella et al., is altered by local syn- and post-depositional faults and associated inter- 2020). nal angular unconformities, although these are not necessarily associ- In the past few years, there has been a renewed interest in shelf ated with major facies changes. The strata also show an abrupt onlap ridges, with several studies that have refined previous depositional termination against a highly-tilted lower Miocene algal limestone unit models (e.g., Snedden et al., 2011; Desjardins et al., 2012; Olariu et al., on top of the basement, formed by Mesozoic rocks from the External 2012; Schwarz, 2012; Messina et al., 2014; Leva-López et al., 2016; Zone (Soria, 1993; Pérez-Valera et al., 2017) (Fig. 2). Michaud and Dalrymple, 2016; Leszczynski and Nemec, 2019; Chiarella et al., 2020). However, most of these studies are from 3. Dataset and methods siliciclastic-dominated systems, and there is a relative lack of studies in mixed (carbonate–siliciclastic) successions, with a few exceptions This study is based on the detailed analysis of a 304 m-thick outcrop of similar deposits described in ancient straits or seaways stratigraphic section (Fig. 3), which was measured at cm-scale. Field (e.g., Longhitano et al., 2012, 2014, 2021; Rossi et al., 2017). In addition, data were obtained using conventional methodology of logging and de- in mixed shallow-marine settings, the carbonate factory is not necessar- scribing sedimentary rocks, collecting information about lithology (tex- ily located close to the coeval shoreline systems supplying the silicic- ture and composition), sedimentary structures, ichnological features lastic fraction (see Schwarz et al., 2018), which can make the correct and composition, bioturbation index (BI of Taylor and Goldring, 1993), identification of isolated shelf sedimentary bodies and their interpreta- orientation of palaeocurrent indicators, scale and geometry of both tion in terms of sequence stratigraphic concepts more complex. stratification and sedimentary bodies, types of contacts and sample col- In this study, an outcrop example from the Upper Miocene of north- lection (n = 7) for thin section and hand-specimen analysis for each ern Guadix Basin (Spain) is presented, with the aim to (i) characterize type of deposit. Once measured, the succession was characterized by de- and discuss the origin of sharp-based mixed carbonate–siliciclastic de- fining sedimentary facies associations and vertical stratigraphic trends. posits in a shallow-marine succession, (ii) propose a depositional and sequence stratigraphic model for their development in an active tec- 4. Results tonic setting, and (iii) provide criteria to adequately differentiate them from their regressive counterparts. 4.1. Facies analysis 2. Geological setting The succession shows a recurrent alternation of coarse and fine- grained mixed carbonate/siliciclastic deposits (Fig. 3), with dominantly The Betic Cordillera represents the northern branch of the arcuate silty marlstones and marly sandstones alternating with m-scale, sharp- Betic-Rif Alpine orogen that closes the westernmost Mediterranean based and laterally-continuous mixed siliciclastic–carbonate medium to Basin (Alboran Basin) across the Gibraltar Arc (Fig. 1). At the beginning coarse-grained packages. A detailed facies analysis has allowed the def- of the Neogene, three major tectono-palaeogeographic domains formed inition of 7 facies associations (FA 1–7), which are described below and and delimited the Betic Cordillera: (1) a fold-and-thrust belt (External summarized in Table 1. Zones or South Iberian Palaeomargin), (2) a thrust stack of metamor- phic nappe complexes (Internal Zones or Alboran Domain), and (3) 4.2. Grey structureless marlstones (FA1-offshore) allochthonous deposits (Flysch or Gibraltar Units) (Balanyá and García-Dueñas, 1987). Westward displacement of the Internal Zones This facies association is composed of whitish grey, structureless to configured two major N–S arcuate thrust systems (Gibraltar and Cazorla faintly laminated marlstones (Fig. 4A, B). Despite the lack of structures, Arcs) connected by E–W transfer fault zones (Pérez-Valera et al., 2017). subtle grain-size changes occur within mm-scale beds, and bedding This structural configuration controlled the creation of high-subsidence contacts are roughly parallel where visible. Thin section analysis reveals depocentres during the Atlantic–Mediterranean connection through that these deposits are dominated by quartz grains and planktonic fora- the Betic corridor (Martín et al., 2009; Hüsing et al., 2010; Reolid et al., minifera, floating inside the muddy matrix that occupies more than 15% 2012). One of these depocentres is found in the Guadix Basin, at the cen- of the rock (Fig. 5A). Other studies have also described sponge spicules tral sector of the Betic Cordillera, which preserves a few hundred-m and radiolarian in the same deposits (Soria, 1993). Beds are mm to cm- thick Tortonian marine succession (Fernández et al., 1996; Soria et al., thick, but packages can reach several metres in thickness (Fig. 6). Large 1999). accumulations of well-preserved bivalves are locally observed in these The study area is located in the northern part of the Guadix Basin deposits in the lower part of the section. Bioturbation is absent to low (Fig. 1). Here the sedimentary infill covers the period from the (BI 0–2). Regional mapping reveals that they form laterally extensive Tortonian to the Quaternary and is composed of six depositional se- units, which can be followed for several km (Figs. 2, 3). Scattered thin- quences (referred to as Units I–VI, after Fernández et al., 1996, bedded (up to 10 cm-thick), normally-graded muddy sandstone beds Fig. 1C), separated by regional unconformities or correlative conformi- are observed within the mudstone successions, some with erosive ties representing major tectonic and/or eustatic events (Fernández bases and rippled tops, and up to moderately bioturbated (BI 0–3). et al., 1996; Soria et al., 1999; García-García et al., 2009). This study is fo- cused on the lowermost part of the succession, with more than 1 km- 4.2.1. Interpretation thick Tortonian marine deposits forming the first three depositional se- The dominant fine-grained nature of these deposits, combined with quences, which are (from base to top): Unit I, the objective of this study, the microfossil content (mainly planktonic foraminifera) and relatively formed by offshore to nearshore silty marlstones, sandstones, low bioturbation index, suggests that they accumulated in a relatively 3 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 river Dehesas de Guadix S E W Unit V Alicún N La Lancha 788 U III Unit II Picacho 818 6.25 Km Trigo Media Fanega 876 959 Cuartillos 954 Unit I Cocón del Buitre 1014 Basement Algal Limestone Studied section (Fig. 3) Fig. 2. Interpreted satellite image of the study area, showing the location of the studied section within the upper Tortonian marine (Units I–III) to continental (Unit V) succession (Soria, 1993). See the marked onlap termination of the lowermost marine deposits (Unit I, objective of this study) into a deformed/tilted Serravalian to lower Tortonian Algal unit (Algal Limestone), on top of a basement formed by Mesozoic to Lower Miocene rocks from the External Zone (Pérez-Valera et al., 2017). A Media Fanega N outcrop SE-NW C 300 Mixed unit (6) Heterolithic Mudstone-prone Mixed unit (5) 250 Heterolithic Mixed unit (4) 200 Heterolithic Mixed unit (3) Heterolithic 150 Mixed unit (2) B Media Fanega N outcrop (interpreted) SE-NW X-X’= ca. 1 km Heterolithic 5 6 (behind outcrop) 4 3 3 100 Mixed unit (1) 2 X Log path X’ Heterolithic 1 post-depositional faults Studied succession Mudstone-prone (Upper Tortonian) 50 Sandstones and 1-6 calcarenites (Mixed units 1-6) Muddy sandstones Algal limestones, marls and evaporites Sand/mud heteroliths (Serravalian - Lower Tortonian) 10 Mudstone (marl) 0m Fig. 3. (A) Uninterpreted and (B) interpreted panoramic view of the Media Fanega North outcrop, the focus of this study. See the alternating succession of upper Tortonian mudstone- prone deposits with several coarser-grained units (1–6). (C) Simplified sedimentary log of the studied succession, showing the location of several sharp-based, mixed clastic-carbonate units (mixed units 1–6), within a succession dominated by muddy sandstone and heterolithic deposits. 4 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Table 1 Summary of the main characteristics of the facies associations recognized in this study. Code Texture Structures Thickness Fossil content Bioturbaon Trace fossils Other Interpretaon Environment Massive to crudely Planktonic organisms: Normally mm-scale Distal offshore seng, below storm wave base, laminated. Subtle grain- foraminifera, sponge spicules and Form regionally-extensive units. Ocasional, thin- Whish grey beds. Form cm- to Absent to low (BI 0- with occasional siliciclasc input by low-density FA1 size changes, diffuse radiolaria. Locally large - bedded (up to 10 cm-thick), normally graded muddy Offshore mudstones. several m-thick 1). turbidity currents and hemipelagic suspension bedding contacts, accummulaon of well-preserved sandstone beds. packages. seling. roughly parallel. bivalves. Grey sandy Absent to 8-40 m-thick Sandstone beds traceable for 100’s of m. Tabular or mudstones, with Typically massive (sandy moderate (BI 0-3). packages (sandy lens shaped, with erosive and/or loaded bases, and Offshore transion seng, above storm-wave. subordinate very mudstones), occasional Vercal or Offshore FA2 mudstones), 5 to 40 Fragments of bivalves. Scolicia. normally graded. Abundance of organic maer, Lower proporon (or preservaon) of storm fine to fine- ripples and HCS horizontal traces, transion cm-thick beds bioclasts and extraclasts (mainly quartz). So- deposits than lower shoreface deposits. grained (sandstones). increase from top (sandstones). sediment deformaon common. sandstones. down. Wavy bedding and Grey sandy symmetrical ripple Isolated cm-thick beds can show so sediment 3-19 m-thick Dominantly low-energy lower shoreface seng. mudstones to laminaon. Occasional Moderate to high deformaon. Paleocurrents from cross-strafied FA3 packages, isolated - - Occasional appearance of combined flow Lower shoreface muddy hummocky, low-angle, (BI 2-4). foresets point dominantly towards the S-SE. Deposits cm-thick beds. deposits during storms. sandstones. tangenal cross- stack forming corsening-up successions. 5 straficaon. Yellow medium to Thalassinoides, Undeformed and sharp-walled burrows, penetrang Transgressive deposits resulng from Abundant skeletal fragments Moderate to high very coarse- 60 to 250 cm-thick Rhizocorallium, up to 20 cm into underlying deposits, and passively remobilizaon of coeval carbonate factory, Transgressive FA4 Structureless. (bivalves, bryozoans, red algae, (BI 3-4). Highly- grained, bioclasc beds. Skolithos, infilled. Organic maer, carbonaceous debris and mixed with ravinement erosion of underlying deposits echinoids), poorly-organized. bioturbated base. calcarenites. Bergaueria. extraclasts (quartz, volcanics). siliciclasc deposits. Planolites, Organic maer, carbonaceous debris and extraclasts Yellow fine to Mixed barforms resulng from the migraon of Structureless to large- 70-150 cm-thick Abundant skeletal fragments Thalassinoides, (quartz, volcanics). Relavely sharp top, occasionally coarse-grained Moderate to high subaqueous bedforms and reworking of FA5 scale, bidireconal beds, grouped in up (bivalves, bryozoans, red algae, Ophiomorpha, cemented and concreonary. Loaded bases Mixed bars bioclasc (BI 3-5). ravinement deposits by shelf processes (i.e. des sigmoidal cross-bedding. to 6 m-thick bedsets echinoids). Bichordites, common. Deposits stacked in single or mulple sets, calcarenites. or storms). Scolicia. with bidireconal accreon towards S-N. Grey-yellow very Up to 20 cm-thick Condensed deposits, formed under low energy, fine to fine- Highly cemented, concreonary horizons, with Condensed FA6 Structurless. beds. Packages up Mainly fragments of bivalves. High (BI 5-6). Scolicia. low sedimentaon rate condions, associated grained ocasional glauconite. deposits to 1.5 m-thick. with regional flooding events. sandstones. Bioclasc, medium Structurless to subtle Concave-up erosive base. Organic maer, Sedimentary Geology 429 (2022) 106077 to coarse-grained Skeletal fragments (bivalves, Low to moderate Subaqueous channel/gulley fills with a regressive FA7 large-scale cross- 5 m-thick package. - carbonaceous debris and large (up to several cm- Channel-fill pebbly bryozoans, red algae). (BI 1-3). surface of marine erosion at the base. bedding. long) extraclasts (quartz, volcanics). sandstones. M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 A B C D E F G FA3-Lower shoreface FA3-Lower shoreface Fig. 4. Field photos of the different facies recognized in the study area. (A) Thick (several m-thick), light grey structureless or faintly laminated mudstones (FA1, offshore). (B) Detail of the subtle lamination in mudstones (FA1, offshore). (C) Example of hummocky-cross stratified sandstone (FA2, offshore transition). (D) Alternating sand/mud heterolithic packages with cm- thick muddy sandstones (FA2, offshore transition). (E) Example of soft-sediment deformation commonly observed in hummocky-cross stratified sandstone (FA2, offshore transition). (F) Coarsening-up heterolithic to muddy sandstone package (FA3, lower shoreface). (G) Wavy-laminated muddy sandstones (FA3, lower shoreface). Field photos of the different facies recognized in the study area. (H) Sharp-based, bioclastic mixed carbonate–clastic bed (FA4, transgressive deposits). (I) Large-scale cross-stratified mixed clastic-carbonate deposits (FA5, mixed bars). (J) Highly bioturbated, cross-stratified mixed clastic-carbonate deposits (FA5, mixed bars). (K) Inset view of (J) showing the coarse-grained and highly bioclastic nature of mixed bar deposits (FA5), with intrabasinal skeletal fragments, extraclasts, and coal fragments. (L) Oxidized, thin-bedded, bioclastic and glauconitic sandstone (FA6, condensed deposits). (M) Detail view of the top surface of a highly bioturbated, bioclastic and glauconitic sandstone (FA6, condensed deposits). (N) Erosive-based, channelized bioclastic medium to coarse grained sandstone deposits (FA7, channel-fill). (O) Inset view of (N) showing the major grain size break across the erosive base of channel-fill deposits (FA7), cutting into lower shoreface muddy sandstones (FA3). 6 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 H I FA4-Transgressive deposits FA5-Mixed bars J K K FA5-Mixed bars FA5-Mixed bars L M FA6-Condensed section FA6-Condensed section N O O Fig. 4 (continued). 7 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 A B Qz MR PF MR Mx PF PF Qz Mx PF Qz BF PF Qz 1 mm PF 1 mm C D Qz Bz CR Bv Qz BF BF CR PF Qz 1 mm 1 mm E F Gt PF PF PF Bz 1 mm 2 cm Fig. 5. Representative thin section (A–E) and close-up (F) photos of the studied deposits. (A) Mudstone-prone facies (FA1, offshore); quartz grains (Qz) and planktonic foraminifera (PF) floating inside the muddy matrix (Mx), that occupies more than 15% of the rock whole. (B) Sandstone levels of heterolithic facies (FA2, offshore transition); densely packed framework formed dominantly by quartz (Qz) with minor metamorphic rocks clasts (MR) and planktonic (PF) and benthic (BF) foraminifera. (C, D, E) Mixed carbonate–siliciclastic unit facies (FA5, mixed bars); quartz grains (Qz) and carbonate rocks fragments (CR), with skeletal fragments including bryozoans (Bz) and bivalves (Bv), with minor planktonic (PF) and benthic (BF) foraminifera, as well as glauconitic grains (Gt). (F) Detail of a hand specimen of carbonate–siliciclastic units facies (FA5, mixed bars), showing the relative abundance of bryozoans (Bz). distal depositional setting, below storm wave base, with dominant low- 4.3.1. Interpretation energy processes such as hemipelagic suspension settling (Birgenheier The heterolithic and coarser-grained character of these facies, to- et al., 2017). Minor presence of normally-graded sandstone thin beds gether with the fossil content (planktonic and benthic foraminifera) suggests that this offshore setting received occasional coarse-grained si- and the common appearance of combined-flow structures suggests liciclastic supply via low-density turbidity currents (e.g., hyperpycnal that these facies accumulated in an offshore transition setting, above flows) (Bhattacharya and MacEachern, 2009; Harazim and McIlroy, storm-wave base (Dott and Bourgois, 1982; Duke, 1985; Duke et al., 2015). 1991; Dumas et al., 2005). Coarse-grained sands were transported by seaward low to high-density turbidity currents (e.g., hyperpycnal 4.3. Heterolithic sandstone/marlstone packages (FA2 - offshore transition) flows), and were partly reworked by storms (e.g., Myrow et al., 2002; Pattison et al., 2007; Lamb et al., 2008; Steel et al., 2018; Jelby et al., This facies association is composed of grey laminated sandy marl- 2020). stones and sandstone/marlstone heterolithic packages, interbedded with 5 to 40 cm-thick isolated fine to coarse-grained sandstone beds 4.4. Wavy-laminated sandy mudstones to muddy sandstones (FA-3 - lower (Fig. 4D). These beds are tabular or lens shaped, with erosive and/or de- shoreface) formed bases (e.g., load casts), normal grading and rippled tops, hummocky-cross stratification and common soft-sediment deforma- This facies association is composed of grey laminated sandy mud- tion (Fig. 4C, E). Naked-eye analysis of sandstone beds reveals abundant stones to muddy sandstones, with wavy bedding and symmetrical extraclasts (mainly quartz), organic matter and bioclasts. Thin section ripple cross-lamination (Fig. 4F, G), and isolated cm-thick beds analysis confirms that they are dominated by quartz grains, with with low-angle, hummocky and tangential/sigmoidal cross stratifi- minor metamorphic rock fragments and planktonic and benthic forami- cation and soft sediment deformation. Palaeocurrents from cross- nifera (Fig. 5B). Tool marks (mainly flutes) and foresets show stratification foresets, where observed, point dominantly towards palaeocurrents ranging to the SW–NW (Fig. 6). Sandstone beds can be the S–SE. Packages are 3 to 19 m-thick, and tend to stack forming up to moderately bioturbated (BI 0–3), with vertical or horizontal traces coarsening-up successions (Fig. 6). They generally display a grada- at the top surface (Fig. 8A). Packages range from 8 to 40 m in thickness tional lower contact from underlying offshore transition deposits (Fig. 6). The tops of these packages can be gradational to overlying (FA2), and are conformably overlain by condensed deposits (FA7) lower shoreface deposits (FA3) or be abruptly truncated by transgres- or abruptly truncated by transgressive (FA4) or channel-fill (FA7) sive deposits (FA4) (Fig. 6). deposits (Fig. 6). 8 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 (m) C3 top TOP SECTION 100 (m) C8 top Symbols / structures TRS Sigmoidal cross-bedding 200 TRS 180 300 g HCS Hummocky cross-strat. g Symmetrical ripples 90 150 Current ripples 190 000 Parallel lamination 290 HCS Normal grading C5 top Plant and micaceous debris 80 180 Mudclasts and intraclasts C2 top 180 Extraclasts (quarz, volcanic, 280 metamorphic rock fragments) TRS Skeletal fragments (bryozoans, red algae, echinoid spicules) HCS Bivalves (fragments) 70 g 170 HCS Bivalves (complete) 270 Bioturbation (poor-intense) Soft-sediment deformation C7 top g Glauconite 60 Paleocurrent (0-359°) HCS 160 TRS Transgressive ravinement HCS 260 295 surface HCS TRS? RSME Regressive surface of 160 242 C4 top marine erosion 50 HCS 170 RSME? 284 150 Lithologies / textures TRS 250 C1 top Muddy calcarenite Calcarenite (cross-bed.) 40 Calcarenite HCS 140 Pebbly sandstone (cross-bed.) 240 Sandstone (cross-bed.) Sandstone HCS HCS Muddy sandstone HCS 30 HCS g Sand/mud heteroliths 130 Sandy mudstone 230 Mudstone (marl) g 288 20 HCS Facies associations (FAs) 120 FA7 220 FA6 Condensed deposits 260 C6 top 180 FA5 Mixed bars Shelf ridge 10 FA4 Transgressive deposits g 110 000 FA3 Lower shoreface 210 TRS FA2 g FA1 g 0 BASE SECTION Fig. 6. Detailed sedimentary log of the studied succession (see location in Fig. 3), showing an alternation of coarse and fine-grained mixed carbonate–siliciclastic deposits, which can be subdivided in at least 8 cycles (C1–C8). 9 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 4.4.1. Interpretation deposits, and are passively infilled by mixed carbonate–clastic sediment The sandy but fine-grained and thin-bedded nature of the deposits, (Fig. 8B, C). This includes abundant skeletal fragments (dominantly common presence of wavy bedding and symmetrical ripples, and occa- from bivalves and bryozoans, and minor red algae and echinoids), or- sional appearance of thick sandstone beds with larger-scale combined- ganic matter, coal fragments and extraclasts (quartz and volcanic-rock flow structures suggest that these deposits accumulated in a domi- fragments), in a relatively poorly-sorted organization. Normally- nantly low-energy lower shoreface setting (Walker and Plint, 1992; graded bed tops occur. These deposits can be laterally discontinuous, Yang et al., 2005; Dumas and Arnott, 2006). but they are commonly found abruptly truncating offshore transition (FA2) or lower shoreface (FA3) deposits, and overlain by mixed bar 4.5. Structureless bioclastic calcarenites (FA4 - transgressive deposits) (FA5) or condensed (FA6) deposits (Figs. 6, 7). This facies association is composed by yellow medium to very 4.5.1. Interpretation coarse-grained, structureless bioclastic calcarenites (Fig. 4H). Beds are The ichnological features found at the base of these deposits allow 60 to 250 cm-thick and moderately to highly bioturbated (BI 3–5) assignation to the Glossifungites ichnofacies, developed into compacted, (Fig. 6). They have a prominent sharp, erosive highly bioturbated base, semi-lithified substrates (Seilacher, 1967). This firmground ichnofacies with vertical, sub-vertical and oblique J-shaped burrows and shallow has been used extensively in the identification of omission surfaces and cylindrical rounded structures, as well as circular sections and horizon- the identification and interpretation of transgressive surfaces tal, branched, forms. Most traces can be assigned to Thalassinoides, but (MacEachern et al., 1992, 1999; Bann et al., 2004; Rodríguez-Tovar with local presence of Rhizocorallium, Skolithos and Bergaueria. Burrows et al., 2007). The contacts are therefore interpreted as transgressive sur- are undeformed and characterized by sharp contacts, showing, in some faces, although evidence is not conclusive to associate them to either cases a penetration depth up to around 20 cm into the underlying wave or tidal ravinement processes (see Cattaneo and Steel, 2003). A B 220 deposits (FA-2) Shelf ridge in B Mixed bars (FA-5) Transgressive ca. 8 m 210 deposits (FA-4) Fig. C Post-depositonal fault 200 urfa ce Fig. C ment s Ravine 190 C Cycle 6 180 m D m) n in A(ca. 40 nt sectio Equivale Fig. 7. Example of the mixed clastic–carbonate units analysed in this study and interpreted as mixed carbonate–clastic shelf ridges. (A) Fragment of the studied section showing the common stratigraphic arrangement of mixed units, abruptly truncating offshore transition (sometimes also lower shoreface) deposits. (B, C) Field example of one of these units, formed by sharp-based skeletal-rich bioclastic calcarenites (FA4), overlain by large-scale sigmoidal cross-bedded calcarenites, forming accreting barforms (FA5). (D) Outcrop photo highlighting the sharp-based, sharp-topped nature of the mixed clastic-carbonate units, as well as their significant lateral extension (outcrop length = ca. 1 km). 10 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 The poorly-sorted and bioclastic-rich deposits immediately overlying minor red algae and echinoids), benthic and planktonic foraminifera, these surfaces are consequently interpreted as transgressive deposits glauconitic grains, organic matter, coal fragment debris and extraclasts (Zecchin et al., 2019), resulting from the remobilization of a coeval car- (Fig. 4K). Thin section and hand-specimen analysis reveals the average bonate factory, mixed with the erosion of underlying offshore transition grain composition is 70% clastic grains (30% quartz, 40% lithic frag- (FA2) and lower shoreface (FA3) deposits. However, the transgressive ments: metamorphic, volcanic and limestone-rock fragments), 10% reworking of coarser-grained, forced-regressive sandstone wedges lo- bioclasts and 20% siliciclastic matrix (Fig. 5C–F). Bars show bidirectional cated farther seaward cannot be ruled out. accretion directions ranging towards the S and N, although southward accretion dominates (Figs. 6, 7). Beds are moderately to highly biotur- 4.6. Sigmoidal cross-bedded bioclastic calcarenites (FA5 - mixed bars) bated (BI 3–5), with traces including dominant Planolites, well- developed Thalassinoides structures, vertical Ophiomorpha shafts, and This facies association is composed of yellow fine to coarse-grained, local Bichordites/Scolicia (Fig. 8D–F). cross-bedded bioclastic calcarenites (Fig. 4I, J). Beds commonly have soft-sediment deformed bases, and are arranged in stacked dominantly 4.6.1. Interpretation single (locally multiple) sets of large-scale sigmoidal cross-bedding, These deposits are interpreted as mixed siliciclastic–carbonate forming up to 8 m-thick barforms (Figs. 6, 7), with relatively sharp barforms, resulting from the reworking of a coeval carbonate factory, to- tops, occasionally highly cemented and concretionary. They have abun- gether with the underlying offshore transition (FA2) and lower dant skeletal fragments (dominantly from bivalves and bryozoans, and shoreface (FA3), but also transgressive deposits (FA4), accumulated A B C D E F G Fig. 8. Examples of trace fossils found in the studied section. (A) Horizontal Ophiomorpha at the upper surface of a storm bed, showing T-shaped branching and pellets along the wall (offshore transition, FA2). (B–C) Vertical, and oblique burrows, as well as circular sections, passively infilled by mixed carbonate–clastic sediments (transgressive deposits, FA4), and penetrating a few cm into the light sandy siltstone deposits below (lower shoreface, FA3). (D) Frequent bioturbation in mixed carbonate–clastic cross beds (mixed bars, FA5), with dominant Planolites and well-developed Thalassinoides structures. (E) Vertical shaft of probable Ophiomorpha (pellets along the wall can be envisaged) (mixed bars, FA5). (F) Bichordites/Scolicia traces showing cross-cutting relationships and similar infilling material than the host mixed carbonate–clastic sediment (mixed bars, FA5). (G) Several traces of Scolicia showing cross-cutting relationships in the upper surface of a bioclastic sandstone bed (condensed section, FA6). 11 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 preferentially in some areas of the seabed (as suggested by their lateral Table 1, Fig. 4L, M) (Fig. 6). These deposits are overlain by poorly- discontinuity), favouring a higher reworking by shelf currents. to moderately-sorted mixed carbonate–clastic units, rich in skeletal fragments and extraclasts (mainly quartz and volcanic fragments), 4.7. Highly bioturbated, concretionary sandstones (FA6 - condensed deposits) and displaying large-scale sigmoidal cross bedding (FA5 – mixed bars, Table 1, Fig. 4I–K). They show a fining- and thinning-up ar- This facies association is composed by grey–yellow, intensely biotur- rangement, often capped by highly-cemented and concretionary bated sandstones (BI 5–6; Fig. 8G), with bioclasts accumulations bioturbated sandstones, with high ichnodiversity (FA6 – condensed (mainly bivalve fragments), occasional glauconitic grains, and often deposits, Table 1, Fig. 4N), interpreted as containing maximum highly cemented or forming concretionary horizons (Fig. 4N, O). Traces flooding surfaces. include Scolicia showing cross-cutting relationships to bed top surfaces (Fig. 8G). Beds are generally thin (up to 20 cm), but packages reach up 6. Depositional model to 1.5 m in thickness. They are often found conformably overlying lower shoreface deposits (FA3) or mixed bars (FA5), and overlain by off- The studied succession is interpreted to have deposited in a rela- shore (FA1) or offshore transition (FA2) fine-grained deposits (Fig. 6). tively shallow-water shelf (Fig. 9), around the storm-wave base, as sug- gested by the relative dominance of offshore transition deposits (FA2) 4.7.1. Interpretation with combined-flow structures (i.e., hummocky cross stratification) The high bioturbation index of these deposits, with multiple gener- (Fig. 6). The fine-grained nature of the coarsening and thickening up ation of traces, together with the presence of bioclast accumulations successions of offshore (FA1), offshore transition (FA2) to lower and glauconitic grains and their concretionary/cemented nature is con- shoreface (FA3) deposits (Fig. 6) suggests that there was a relatively dis- sistent with condensed deposits; these represent a considerable span of tal coeval west- to north-westward prograding shoreline system time recorded by only relatively thin layers, and form under low energy, (Fig. 10a). This shelf was only receiving occasional coarse-grained silic- low sedimentation rate conditions, associated with increased water iclastic sediment supply (and organic debris) via forced regressions depth during regional flooding events (Loutit et al., 1988). and/or seaward gravity flows (e.g. hyperpycnal flows), which under- went storm reworking during or shortly after deposition, and resulted 4.8. Erosive-based, bioclastic pebbly sandstones (FA7 - channel-fill) in discrete cm-thick sandstone beds within offshore transition deposits (Fig. 10b). After enough time to create a firm or compacted substrate, This facies association is composed of bioclastic, cross-bedded peb- offshore transition to lower shoreface deposits were partially eroded bly sandstones, contained in a concave-up erosive base, cutting several during transgression, with the development of erosive and highly bio- cm into the underlying deposits, and forming a 5 m-thick package turbated ravinement surfaces (Fig. 10c), as suggested by the unde- (Fig. 4L). The package is slightly fining-up, and contains a mix of skeletal formed and sharp nature of the burrows (Fig. 8B, C) and their fragments (dominantly bivalves, but also bryozoans and red algae), or- association to Glossifungites ichnofacies. These ravinement surfaces ganic matter and large (up to several cm-long) angular extraclasts were followed by deposition of a relatively poorly-sorted assemblage (quartz and volcanic fragments), more concentrated towards the base of mixed deposits (FA4), dominated by skeletal fragments resulting (Fig. 4M). This facies association is only recognized in the upper part from the remobilization of a coeval carbonate factory (Fig. 10d). The un- of the studied section, abruptly truncating lower shoreface deposits even accumulation of these mixed deposits on the seabed possibly re- (FA3), and overlain by mixed bars (FA5) (Fig. 6). sulted in areas that favoured higher reworking via shelf (most likely storm-wave) processes and nucleation of laterally extensive shelf 4.8.1. Interpretation ridges, with the development of sigmoidal cross-bedded barforms The highly erosive, concave-up basal surface, together with the (FA5) (Fig. 10e). These show bidirectional accretion orientations (N– coarser nature and larger presence of landward material, mixed with S), but dominantly pointing southward, at a high angle with respect to reworked skeletal fragments, is consistent with these deposits being the dominantly west- to north-westward orientation of unidirectional interpreted as subaqueous channel fills (Fig. 6). palaeocurrents recorded from offshore-transition deposits (Fig. 9B). Continued transgression resulted in regional flooding, increased water 5. Stratigraphic arrangement depth and a decrease of reworking processes and deposition, leading to lower sedimentation rates and the development of highly The studied succession is summarized in Fig. 6. The succession biortubated, condensed deposits (FA7), containing maximum flooding shows an alternation of coarse and fine-grained mixed carbonate–silic- surfaces (Fig. 10f). Finally, the next phase of advancement of the regres- iclastic deposits, which can be subdivided in at least 8 progradational– sive shoreline system led to progressive deposition of fine-grained sed- retrogradational cycles (C1–C8), each of them 23 to 45 m-thick iments in offshore and offshore-transition settings, resulting in the (Figs. 3, 5). Cycles start with either dominantly structureless to faintly burial and effective preservation of the underlying mixed carbonate–si- laminated marlstones, with occasional thin-bedded sandstones, some liciclastic shelf ridges (Fig. 10g). with erosive bases and rippled tops (FA1 – offshore, Table 1, Fig. 4A), or with an alternation of laminated sandy marlstones and medium- 7. Discussion bedded sandstones, with hummocky-cross stratification and common soft-sediment deformation (FA2 – offshore transition, Table 1, Fig. 4C, 7.1. A fine-grained siliciclastic shelf and the origin of the remobilized D). In some cycles (C1–3 and C7–8, Fig. 6), these are progressively re- carbonate factory placed by coarsening-up packages of sandy mudstones to muddy sand- stones, with wavy bedding and symmetrical ripple cross-lamination In the studied succession, the fine-grained, siliciclastic dominated (FA3 – lower shoreface, Table 1, Fig. 4E). This progradational stacking offshore to lower shoreface deposits (FA1–FA3, Table 1) are abruptly culminates in some cycles (C1–2, Fig. 6) with thin, intensely bioturbated truncated by mixed carbonate–siliciclastic units, through sharp, highly sandstones (FA6 – condensed deposits, Table 1, Fig. 4N). In other cycles bioturbated transgressive ravinement surfaces. These mixed deposits (C3–8, Fig. 6), it is abruptly truncated by erosive contacts bioturbated by are remarkably different from the underlying shelf deposits, with large, sharp-walled burrows, passively infilled by overlying mixed car- coarse-grained, bioclastic calcarenites (FA4, FA5, Table 1) with skeletal bonate–clastic sediments (FA4 – transgressive deposits, Table 1, fragments. Because these skeletal fragments are only recognized in the Fig. 4H), or in just one occasion by concave-up erosive surfaces, filled mixed clastic–carbonate units (see Fig. 5), this implies the presence of with bioclastic cross-bedded pebbly sandstones (FA6 – channel fill, a coeval carbonate factory, located in either (i) a more distal position 12 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 A N B N Re gr es siv es ho W E re f ac e y Studa n = 13 s are f ridge S shel ssive sgre Tran C Condensed section (MFS) tran Shelf ridge sgr. (FA4-5) Transgressive ravinement surface (TRS) ssive (FA2) to lower Storm beds regre shoreface (FA3) Marlstones Fig. 9. (A) Depositional model, (B) palaeocurrent distribution (coloured according to the FA codes) and (C) simplified cycle of the sharp-based mixed carbonate–clastic shallow-marine deposits recognized in the studied succession. See text for more details. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) or (ii) a lateral position within the shelf. The occurrence of a bryomol- conditions induced by persistent storm-wave action. This is more char- type skeletal association in the mixed deposits (mainly bryozoans acteristic around the shoreface zone than in more distal offshore set- and bivalves, and minor red algae and echinoids), would indicate tings (van Heteren et al., 2011; Rossi et al., 2017), where tidally- non-tropical, temperate-type shallow-water conditions (Betzler modulated segregation commonly occurs (Chiarella et al., 2012). The et al., 1997). Because of the relative dominance of siliciclastic mate- textural nature of the studied shelf ridges, more poorly-sorted and rial of the studied mixed deposits it is not possible to reconstruct a coarser-grained than conventional tidal-dominated offshore ridges, biofacies belt model as described in other shallow-marine examples would therefore suggest that they developed around the shoreface richer in carbonate skeletal-grains (e.g., late Miocene ramp of zone, where sediment reworking by storm waves was common. The Menorca, Spain, Pomar et al., 2012). However, bryozoan–mollusc– abundant extrabasinal detrital material derived from the high-energy echinoid associations have been reported as dominant in storm reworking of (i) forced-regressive coarse-grained sandstones carbonate factories located at the proximal sector of the outer ramp and (ii) sediment gravity-flow deposits, as extraclasts and terrestrial or- (Brandano and Corda, 2002). This biota association is therefore char- ganic debris is commonly observed in sandstone beds within lower acteristic of deeper depositional environments (i.e., aphotic zone in shoreface and offshore transition deposits (Fig. 5B). Additionally, well- outer-middle ramp, Brandano and Corda, 2002) compared to developed burrowed ravinement basal surfaces and relatively short other skeletal associations, like branching red algae-dominant ridges (with single cross-bedding sets, and not forming compound (i.e., oligophotic zone - middle ramp) identified in other time- bars) are more characteristic of gentle slopes and shallower-water set- equivalent successions in the nearby Tabernas Basin (García-García tings (i.e., shoreface) (Nnafie et al., 2014). et al., 2006b). This is therefore considered to favour the interpreta- Simulations of sand ridges with morphodynamic models conclude tion that the coeval carbonate factory supplying the skeletal frag- that the morphology and activity of sand ridges are controlled by the ments was located farther offshore, and remobilized during rate of sea-level rise, depth and coastal-shelf slope (Nnafie et al., transgressions. The scenario where the carbonate factory is located 2014). Following those models, the shelf ridges studied here, with in more distal positions relative to the equivalent shoreline supply- more common examples of single than compound barforms, would ing the siliciclastic fraction can occur quite commonly in mixed car- have been enhanced during low rates of sea-level rise on gentle coastal bonate–siliciclastic shallow-marine systems (Schwarz et al., 2018; to inner shelf slopes. Marine transgressions represent common scenar- see also Reijmer, 2021). ios for the development of mixed carbonate–siliciclastic shelves (García-García et al., 2006b; Fontana et al., 2015; Salocchi et al., 2017), 7.2. Poorly-sorted versus well-sorted shelf ridges where the interplay of high-energy currents removing carbonate facto- ries and coming from detrital input drowning emerged areas encour- Several of the mixed carbonate–siliciclastic deposits in the studied ages the mixing of carbonate and siliciclastic grains (Longhitano et al., section are relatively poorly sorted and contain abundant extraclasts 2014). (mainly quartz and lithic fragments) and terrestrial organic matter frag- ments (Fig. 5). This contrasts with conventional transgressive shelf 7.3. Implications for other studies of sharp-based shallow-marine deposits ridges, mostly composed of well-sorted sandstones (Cattaneo and Steel, 2003), particularly those undergoing long-term reworking/ The sharp bases of the mixed carbonate–siliciclastic deposits studied remoulding during their migration along the shelf (Snedden and here, assigned to the Glossifungites ichnofacies, have been associated Dalrymple, 1999). The absence of an efficient segregation of heterolithic with compacted, semi-lithified substrates, and interpreted as transgres- grains in the studied mixed shelf ridges is consistent with high-energy sive surfaces in other studies (Seilacher, 1967; MacEachern et al., 1992, 13 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 a) Normal regression of 7.4. The influence of basin configuration in the upper Tortonian of the Betic siliciclastic-starved shelf Corridor long-term process One of the most characteristic features of the studied succession is the repetition of offshore/shoreface siliciclastic- and shelf mixed- b) Deposition / reworking of hyperpicnites or lithofacies into 8 cycles (C1–8, see Fig. 6). The consistency of the oscilla- forced regressive sandstone wedges tion between similar depositional environments throughout the section suggests similar water depths and hydrodynamic regime persisted through time. A balanced accommodation/sediment supply ratio, with constant sediment supply and tectonic subsidence creating continuous c) Transgressive ravinement erosion accommodation space, would explain the preservation of such a thick, aggradational succession. However, other studies in relatively time- equivalent deposits in the southern margin of the Guadix Basin and in the northern margin of the Guadalquivir Foreland Basin have demon- strated the existence of coeval net regressive, siliciclastic-dominated short-term process shoreline systems (García-García et al., 2006a, 2021). These studies ev- and deposition of mixed deposits idence the existence of a complex and dynamic basin configuration in the upper Tortonian, with the development of local depocentres and relatively narrow corridors or seaways during the connection between the Mediterranean and Atlantic (Martín et al., 2009; Reolid et al., 2012). This configuration resulted in intensification of bottom currents e) Reworking of mixed deposits and nucleation of shelf ridges and favoured shelf reworking processes, as seen in this study and also in younger deposits (Betzler et al., 2006; García-García et al., 2009), and in the nearby Rifian corridor (Capella et al., 2017; de Weger et al., 2020; Beelen et al., 2021; Miguez-Salas et al., 2021). But it also pro- moted the development of local sediment entry points and variable stacking patterns, reflecting a differential interaction between active of condensed surface tectonics and sedimentation across the region (e.g., Andrić et al., 2018). long-term process 8. Conclusions g) Renewed advancement of regressive This study analyses and discusses the origin and development of shoreline, burial and preservation sharp-based, mixed carbonate–siliciclastic shallow-marine deposits, with an outcrop example from the Upper Miocene of the Betic Cordillera (Spain). These mixed deposits abruptly truncate siliciclastic-dominated offshore to lower shoreface facies, via sharp, highly bioturbated contacts interpreted as transgressive ravinement surfaces, and form several m- Fig. 10. Proposed evolutionary model for the development and preservation of sharp- thick and hundreds of m-long depositional elements, interpreted as based, mixed carbonate–clastic shallow-marine deposits, interpreted as transgressive mixed carbonate–clastic shelf ridges. These ridges formed in a fine- shelf ridges. See text for a more detailed description of the different stages (a–f). grained shelf which received occasional coarse siliciclastic supply via sediment gravity flows, but with a coeval offshore carbonate factory, 1999; Bann et al., 2004; Rodríguez-Tovar et al., 2007). This, combined eroded and remobilized during transgressions. Similar sharp-based with the presence of skeletal fragments from an offshore carbonate fac- shallow-marine deposits could be tentatively misinterpreted as tory, significantly different from the underlying offshore transition to forced-regressive wedges in other studies. However, this work provides lower shoreface siliciclastic deposits, and the fining, thinning-up stack- criteria to distinguish them, including the nature of their lower contact, ing of the deposits is consistent with these mixed units being presence of reworked offshore skeletal fragments and their stacking interpreted as transgressive deposits (Fig. 9C). Several studies have pro- pattern, which are consistent with their interpretation as transgressive posed the sharp-based coarser-grained nature of some isolated deposits. When put in context with other studies in relatively time- shallow-marine deposits as criteria to interpret them as incised-valley equivalent regressive and more siliciclastic-dominated successions fills or forced-regression sandstone wedges, associated with abrupt nearby, this evidences a complex configuration of the Mediterranean– lowerings of relative sea-level (e.g. Hunt and Tucker, 1992; Ainsworth Atlantic connection during the upper Miocene, with sea corridors in- et al., 2000; Fitzsimmons and Johnson, 2000; Posamentier and Morris, creasing currents and shelf reworking processes, and local sediment 2000; García-García et al., 2011). These studies document significant supplies and depocentres resulting in laterally variable stacking grain-size breaks across sharp boundaries, but do not focus on signifi- patterns, and reflecting differential and complex tectono-sedimentary cant compositional changes across major contacts. Therefore, our interactions. study emphasizes the importance of a careful analysis of the geometry and ichnology of sharp basal contacts in shallow-marine deposits, but Declaration of competing interest also potential differential composition across their boundaries, and their stacking pattern, as key criteria to differentiate transgressive The authors declare that they have no known competing financial sharp-based mixed carbonate–siliciclastic deposits from their regres- interests or personal relationships that could have appeared to influ- sive counterparts. Adequately determining the correct depositional ence the work reported in this paper. model for the development of sharp-based, shallow-marine deposits detached from their coeval coastline and encased in marine mudstones Acknowledgements is critical as different interpretations may imply significant differences in their predicted reservoir performance (Snedden and Bergman, This work was supported by Aker BP (ShelfSed project, University of 1999; Cattaneo and Steel, 2003). Oslo) and Agencia Estatal de Investigación (AEI) y Fondo Europeo de 14 M. Poyatos-Moré, F. García-García, F.J. Rodríguez-Tovar et al. Sedimentary Geology 429 (2022) 106077 Desarrollo Regional (FEDER) (CGL2017-89618-R project, University of Duke, W.L., 1985. Hummocky cross-stratification, tropical hurricanes, and intense winter storms. Sedimentology 32, 167–194. Granada). The study by RT was funded by the project PID2019- Duke, W.L., Arnott, R.W.C., Cheel, R.J., 1991. Shelf sandstones and hummocky cross- 104625RB-100 (Secretaría de Estado de I+D+I, Spain), Research Group stratification: new insights on a stormy debate. Geology 19, 625–628. RNM-178 (Junta de Andalucía), B-RNM-072-UGR18 (FEDER Andalucía), Dumas, S., Arnott, R.W.C., 2006. Origin of hummocky and swaley cross-stratification—the controlling influence of unidirectional current strength and aggradation rate. Geology and P18-RT-4074 (Junta de Andalucía), and the Scientific Excellence 34, 1073–1076. Unit UCE-2016-05 (Universidad de Granada). The study by JS was Dumas, S., Arnott, R.W.C., Southard, J.B., 2005. Experiments on oscillatory-flow and funded by the project PID2020-114381GB-100 (Secretaría de Estado combined-flow bed forms: implications for interpreting parts of the shallow- de I+D+I, Spain). marine sedimentary record. Journal of Sedimentary Research 75, 501–513. Dyer, K.R., Huntley, D.A., 1999. The origin, classification and modelling of sand banks and ridges. 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