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Fig. 7. Las Mingachas. A) Outcrop view of the basinal transgressive marls of the Forcall Formation (lower Aptian). Depositional Sequence A. Hammer = 32 cm. B) Matrix-supported texture with fragments of molluscs. Transgressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. C) Packstone texture with Palorbitolina lenticularis of the upper, transgressive part of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. D) Photomicrograph of a specimen of Palorbitolina lenticularis? showing the embryonic apparatus. Highstand normal regressive marly-limestones of the Forcall For- mation (lower Aptian). Depositional Sequence A. Scale = 1 mm. E) Photomicrograph of a specimen of Praeorbitolina cormyi showing the embryonic apparatus. Highstand normal regressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. F) Dufrenoyia sp. Highstand normal regressive marly-limestone deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Visible part of pencil = 3.9 cm. See Fig. 4 for locations.

Figure 7 Las Mingachas. A) Outcrop view of the basinal transgressive marls of the Forcall Formation (lower Aptian). Depositional Sequence A. Hammer = 32 cm. B) Matrix-supported texture with fragments of molluscs. Transgressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. C) Packstone texture with Palorbitolina lenticularis of the upper, transgressive part of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. D) Photomicrograph of a specimen of Palorbitolina lenticularis? showing the embryonic apparatus. Highstand normal regressive marly-limestones of the Forcall For- mation (lower Aptian). Depositional Sequence A. Scale = 1 mm. E) Photomicrograph of a specimen of Praeorbitolina cormyi showing the embryonic apparatus. Highstand normal regressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. F) Dufrenoyia sp. Highstand normal regressive marly-limestone deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Visible part of pencil = 3.9 cm. See Fig. 4 for locations.

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Fig. 1. A) Geographical location of the study area in the eastern Iberian Chain (E Iberia). B) Simplified isopach and structural map of the Maestrat Basin during the Late Jurassic and Early Cretaceous rifting cycles and location of the study localities in the Galve Sub-basin. The location of outcrops discussed in the paper are also indicated. Mo: Morella Sub-basin, Pe: El Perell6 Sub-basin, Sa: La Salzedella Sub-basin, Ga: Galve Sub-basin, Ol: Oliete Sub-basin, Pa: Las Parras Sub-basin, Ce: Cedraman Sub-basin, Or: Orpesa Sub-basin, Pg: Penyagolosa Sub-basin. Modified after Salas et al. in Martin-Chivelet et al. (2019). The situation of the Campello Fault is taken from Martin-Martin et al. (2015). C) Geological map of the central Galve Sub-basin. The outcrops studied and discussed in the paper are respectively indicated with red and blue stars. Modified after Canérot et al. (1979) and Gautier (1980). The conceptual cross-section A-A’ is shown in Fig. 3C. Universal Transverse Mercator (UTM) Projection: Zone 30, Datum ETRS89. UTM coordinates are written in km. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) factors could have also acted in combination or isolated giving rise to the Davies et al., 2020; Simmons et al., 2020). However, alternative mechanisms capable of triggering sea-level fluctuations of this order include regional- to plate-scale tectonic processes, interactions between mantle and lithosphere, formation of large igneous provinces, thermo- eustasy, aquifer-eustasy, and variations in the volume of mid-oceanic ridges and sediment supply (e.g., Hay and Leslie, 1990; Cloetingh, 1991; Cronin, 1999; Immenhauser, 2005; Conrad, 2013; Haq, 2014; Cloetingh and Haq, 2015; Sames et al., 2016, 2020; Wendler and Wendler, 2016; Wendler et al., 2016; Li et al., 2018). Such potential factnre eniild have alen acted in ecambhination nar ienlated civino rice tn the
Fig. 1. A) Geographical location of the study area in the eastern Iberian Chain (E Iberia). B) Simplified isopach and structural map of the Maestrat Basin during the Late Jurassic and Early Cretaceous rifting cycles and location of the study localities in the Galve Sub-basin. The location of outcrops discussed in the paper are also indicated. Mo: Morella Sub-basin, Pe: El Perell6 Sub-basin, Sa: La Salzedella Sub-basin, Ga: Galve Sub-basin, Ol: Oliete Sub-basin, Pa: Las Parras Sub-basin, Ce: Cedraman Sub-basin, Or: Orpesa Sub-basin, Pg: Penyagolosa Sub-basin. Modified after Salas et al. in Martin-Chivelet et al. (2019). The situation of the Campello Fault is taken from Martin-Martin et al. (2015). C) Geological map of the central Galve Sub-basin. The outcrops studied and discussed in the paper are respectively indicated with red and blue stars. Modified after Canérot et al. (1979) and Gautier (1980). The conceptual cross-section A-A’ is shown in Fig. 3C. Universal Transverse Mercator (UTM) Projection: Zone 30, Datum ETRS89. UTM coordinates are written in km. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) factors could have also acted in combination or isolated giving rise to the Davies et al., 2020; Simmons et al., 2020). However, alternative mechanisms capable of triggering sea-level fluctuations of this order include regional- to plate-scale tectonic processes, interactions between mantle and lithosphere, formation of large igneous provinces, thermo- eustasy, aquifer-eustasy, and variations in the volume of mid-oceanic ridges and sediment supply (e.g., Hay and Leslie, 1990; Cloetingh, 1991; Cronin, 1999; Immenhauser, 2005; Conrad, 2013; Haq, 2014; Cloetingh and Haq, 2015; Sames et al., 2016, 2020; Wendler and Wendler, 2016; Wendler et al., 2016; Li et al., 2018). Such potential factnre eniild have alen acted in ecambhination nar ienlated civino rice tn the
Fig. 2. Chrono-stratigraphic chart for the latest Barremian-Aptian of the Galve Sub-basin. The chrono-stratigraphic chart includes major transgressive- regressive sequences (modified from Bover-Arnal et al., 2016) and deposi- tional sequences interpreted in this study. The ammonoid zonation is taken from Reboulet et al. (2018). The ammonite zones identified in the Maestrat Basin are highlighted in grey.
Fig. 2. Chrono-stratigraphic chart for the latest Barremian-Aptian of the Galve Sub-basin. The chrono-stratigraphic chart includes major transgressive- regressive sequences (modified from Bover-Arnal et al., 2016) and deposi- tional sequences interpreted in this study. The ammonoid zonation is taken from Reboulet et al. (2018). The ammonite zones identified in the Maestrat Basin are highlighted in grey.
Fig. 4. Sedimentary log of the lower Aptian succession of Las Mingachas including the forced regressive unit interpreted and its underlying highstand normal regressive and transgressive deposits, as well as its overlying lowstand normal regressive strata. The stratigraphic section displays the sequence-stratigraphy analysis, the stratigraphic position of the samples collected, the lithostratigraphic units, the lithologies, the bedding, the textures, the sedimentary features, the location of Figs. 7 and 8A-D, and the stratigraphic position of the skeletal and non-skeletal components identified. See Figs. 3 and 5 for location of the section.
Fig. 4. Sedimentary log of the lower Aptian succession of Las Mingachas including the forced regressive unit interpreted and its underlying highstand normal regressive and transgressive deposits, as well as its overlying lowstand normal regressive strata. The stratigraphic section displays the sequence-stratigraphy analysis, the stratigraphic position of the samples collected, the lithostratigraphic units, the lithologies, the bedding, the textures, the sedimentary features, the location of Figs. 7 and 8A-D, and the stratigraphic position of the skeletal and non-skeletal components identified. See Figs. 3 and 5 for location of the section.
Fig. 5. Las Mingachas. A) Outcrop photograph of the sedimentary wedge interpreted as a forced regressive unit. B) Interpretation of Fig. 5A including the lithos- tratigraphic units, the sequence stratigraphic framework, and the stratigraphic log shown in Fig. 4. Note the sharp nature of the interpreted basal surface of forced regression and correlative conformity (sequence boundary). a = altitude. Inset: scale bar = 1 m. Modified from Bover-Arnal et al. (2009). C) Outcrop view of the lower part of the sedimentary log shown in Fig. 4. D) Interpretation of Fig. 5C including the lithostratigraphic units and the sequence stratigraphic framework. Jacob’s staff = 1.5 m. See Fig. 3 for key.
Fig. 5. Las Mingachas. A) Outcrop photograph of the sedimentary wedge interpreted as a forced regressive unit. B) Interpretation of Fig. 5A including the lithos- tratigraphic units, the sequence stratigraphic framework, and the stratigraphic log shown in Fig. 4. Note the sharp nature of the interpreted basal surface of forced regression and correlative conformity (sequence boundary). a = altitude. Inset: scale bar = 1 m. Modified from Bover-Arnal et al. (2009). C) Outcrop view of the lower part of the sedimentary log shown in Fig. 4. D) Interpretation of Fig. 5C including the lithostratigraphic units and the sequence stratigraphic framework. Jacob’s staff = 1.5 m. See Fig. 3 for key.
Fig. 8. Las Mingachas. A) Detail of a poorly preserved rudist section present in the highstand normal regressive marly-limestones of the Forcall Formation (lowe Aptian). Note the presence of orbitolinids (0). Depositional Sequence A. Visible part of pencil = 3 cm. B) Packstone of benthic foraminifera (bf) and abrade: ragments of Permocalculus (P) belonging to the highstand normal regressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = ° nm. C) Grainstone texture containing specimens of Orbitolinopsis (Os) and a section of Marinella lugeoni (MI) of the middle part of the forced regressive wedge Villarroya de los Pinares Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. D) Microphotograph of the forced regressive deposits exhibiting ; srainstone texture with intraclasts (I) and a specimen of Orbitolinopsis (Os). Villarroya de los Pinares Formation (lower Aptian). Depositional Sequence A. Scale = ° mm. See Fig. 4 for locations. E) Outcrop view of the transgressive marls of the lower part of the Benassal Formation overlying drowned transgressive platform toy carbonates belonging to the Villarroya de los Pinares Formation (uppermost lower Aptian). Depositional Sequence B. Encircled ruler = 15 cm. See Figs. 3 and 6C fo <ey and location, respectively. F) Close-up view of the drowning surface located at the top of the transgressive platform carbonates of the Villarroya de los Pinare “ormation (uppermost lower Aptian). This ferruginous and perforated surface corresponds to a hardground. Depositional Sequence B. Width of image = c. 25 cm. Se ‘igs. 6C and 8E for location.
Fig. 8. Las Mingachas. A) Detail of a poorly preserved rudist section present in the highstand normal regressive marly-limestones of the Forcall Formation (lowe Aptian). Note the presence of orbitolinids (0). Depositional Sequence A. Visible part of pencil = 3 cm. B) Packstone of benthic foraminifera (bf) and abrade: ragments of Permocalculus (P) belonging to the highstand normal regressive deposits of the Forcall Formation (lower Aptian). Depositional Sequence A. Scale = ° nm. C) Grainstone texture containing specimens of Orbitolinopsis (Os) and a section of Marinella lugeoni (MI) of the middle part of the forced regressive wedge Villarroya de los Pinares Formation (lower Aptian). Depositional Sequence A. Scale = 1 mm. D) Microphotograph of the forced regressive deposits exhibiting ; srainstone texture with intraclasts (I) and a specimen of Orbitolinopsis (Os). Villarroya de los Pinares Formation (lower Aptian). Depositional Sequence A. Scale = ° mm. See Fig. 4 for locations. E) Outcrop view of the transgressive marls of the lower part of the Benassal Formation overlying drowned transgressive platform toy carbonates belonging to the Villarroya de los Pinares Formation (uppermost lower Aptian). Depositional Sequence B. Encircled ruler = 15 cm. See Figs. 3 and 6C fo <ey and location, respectively. F) Close-up view of the drowning surface located at the top of the transgressive platform carbonates of the Villarroya de los Pinare “ormation (uppermost lower Aptian). This ferruginous and perforated surface corresponds to a hardground. Depositional Sequence B. Width of image = c. 25 cm. Se ‘igs. 6C and 8E for location.
Fig. 9. Barranco de la Canal. A) Drone-based photogrammetric model of the deeply incised erosional surface bounding highstand platform top carbonates o: Depositional Sequence A from the overlying transgressive limestones, which back-fill an incised valley, of Depositional Sequence B above. B) Interpretation of Fig. 9A including the lithostratigraphic units and the sequence-stratigraphic interpretation after Bover-Arnal et al. (2009). Note the stepped nature of the incision surface Note also the drowning of the higher-energy transgressive unit of the uppermost Villarroya de los Pinares Formation and how it is buried by marls of the lower part o: the Benassal Formation. See Figs. 3 and 1C for key and location, respectively. The drone-based photogrammetric model is courtesy of Riccardo Rocca and available a http://riccardorocca.github.io/home/Camarillas_Platform.html, accessed 11 September 2021).
Fig. 9. Barranco de la Canal. A) Drone-based photogrammetric model of the deeply incised erosional surface bounding highstand platform top carbonates o: Depositional Sequence A from the overlying transgressive limestones, which back-fill an incised valley, of Depositional Sequence B above. B) Interpretation of Fig. 9A including the lithostratigraphic units and the sequence-stratigraphic interpretation after Bover-Arnal et al. (2009). Note the stepped nature of the incision surface Note also the drowning of the higher-energy transgressive unit of the uppermost Villarroya de los Pinares Formation and how it is buried by marls of the lower part o: the Benassal Formation. See Figs. 3 and 1C for key and location, respectively. The drone-based photogrammetric model is courtesy of Riccardo Rocca and available a http://riccardorocca.github.io/home/Camarillas_Platform.html, accessed 11 September 2021).
Fig. 11. Barranco de la Canal, Campillo Bajo and Camino de Camarillas. A) View and interpretation of the Camino de Camarillas outcrop including the composite sequence boundary (SU + TS), which separates subaerially exposed highstand platform carbonates below from transgressive strata above. In this outcrop, the subaerial unconformity exhibits a flat erosional profile. Encircled ruler = 15 cm. See Figs. 3 and 1C for key and location, respectively. B) Outcrop view and interpretation of the uppermost Villarroya de los Pinares Formation made up of transgressive grainstones exhibiting cross-bedding with local herring-bone structures. Note the drowning surface at the top of these higher-energy carbonates. Campillo Bajo. See Fig. 10B for location. See Fig. 3 for key. C) Photomicrograph of a grainstone texture rich in oysters (O), which is the most representative microfacies of the transgressive higher-energy unit of Depositional Sequence B. Note also the presence of intraclasts (I) and of a section of coral (C). Barranco de la Canal. See Fig. 9B for location. Scale = 1 mm. D) Close-up view of palaeokarst features found at the top of highstand normal regressive carbonates of the Villarroya de los Pinares Formation. Camino de Camarillas. See Fig. 11A for location. Visible part of pencil = 12 cm. E) Detail of the palaeokarst infilling, which locally includes coarse fragments of echinoid spines and bivalve shells. Campillo Bajo. Visible part of pencil = 2.5 cm. F) Close-up view of the composite sequence boundary showing the subaerial unconformity (SU) with palaeokarst features and the superposed transgressive surface (TS), which corresponds to a rockground exhibiting Gastrochaenolites. Campillo Bajo. See Fig. 3 for key. Pencil = 15 cm.
Fig. 11. Barranco de la Canal, Campillo Bajo and Camino de Camarillas. A) View and interpretation of the Camino de Camarillas outcrop including the composite sequence boundary (SU + TS), which separates subaerially exposed highstand platform carbonates below from transgressive strata above. In this outcrop, the subaerial unconformity exhibits a flat erosional profile. Encircled ruler = 15 cm. See Figs. 3 and 1C for key and location, respectively. B) Outcrop view and interpretation of the uppermost Villarroya de los Pinares Formation made up of transgressive grainstones exhibiting cross-bedding with local herring-bone structures. Note the drowning surface at the top of these higher-energy carbonates. Campillo Bajo. See Fig. 10B for location. See Fig. 3 for key. C) Photomicrograph of a grainstone texture rich in oysters (O), which is the most representative microfacies of the transgressive higher-energy unit of Depositional Sequence B. Note also the presence of intraclasts (I) and of a section of coral (C). Barranco de la Canal. See Fig. 9B for location. Scale = 1 mm. D) Close-up view of palaeokarst features found at the top of highstand normal regressive carbonates of the Villarroya de los Pinares Formation. Camino de Camarillas. See Fig. 11A for location. Visible part of pencil = 12 cm. E) Detail of the palaeokarst infilling, which locally includes coarse fragments of echinoid spines and bivalve shells. Campillo Bajo. Visible part of pencil = 2.5 cm. F) Close-up view of the composite sequence boundary showing the subaerial unconformity (SU) with palaeokarst features and the superposed transgressive surface (TS), which corresponds to a rockground exhibiting Gastrochaenolites. Campillo Bajo. See Fig. 3 for key. Pencil = 15 cm.
Fig. 12. Loma de Camarillas. A) Panoramic view of the lower part of the succession studied. B) Interpretation of Fig. 12A including the lithostratigraphic units, the sequence-stratigraphic framework, and the location of figs. 12C-D and the lower part of the stratigraphic log shown in Fig. 13. Width of image = c. 200 m. C) Panoramic view of the upper part of the succession studied, which belongs to the Benassal Formation. D) Interpretation of Fig. 12C including the sequence- stratigraphic framework, and the location of figs. 14B-F and the upper part of the stratigraphic log shown in Fig. 13. Width of image = c. 60 m. See Fig. 3 for key.
Fig. 12. Loma de Camarillas. A) Panoramic view of the lower part of the succession studied. B) Interpretation of Fig. 12A including the lithostratigraphic units, the sequence-stratigraphic framework, and the location of figs. 12C-D and the lower part of the stratigraphic log shown in Fig. 13. Width of image = c. 200 m. C) Panoramic view of the upper part of the succession studied, which belongs to the Benassal Formation. D) Interpretation of Fig. 12C including the sequence- stratigraphic framework, and the location of figs. 14B-F and the upper part of the stratigraphic log shown in Fig. 13. Width of image = c. 60 m. See Fig. 3 for key.
Fig. 13. Sedimentary log of the lower upper Aptian succession of Loma de Camarillas including depositional sequences B and C. The stratigraphic section displays th sequence-stratigraphic analysis, the stratigraphic position of the samples collected, the lithostratigraphic units, the lithologies, the bedding, the textures, the sed mentary features, the location of figs. 14A-F, and the stratigraphic position of the skeletal and non-skeletal components identified. See Fig. 12 for location of th section. See Figs. 3-4 for key.
Fig. 13. Sedimentary log of the lower upper Aptian succession of Loma de Camarillas including depositional sequences B and C. The stratigraphic section displays th sequence-stratigraphic analysis, the stratigraphic position of the samples collected, the lithostratigraphic units, the lithologies, the bedding, the textures, the sed mentary features, the location of figs. 14A-F, and the stratigraphic position of the skeletal and non-skeletal components identified. See Fig. 12 for location of th section. See Figs. 3-4 for key.
Fig. 14. Loma de Camarillas. A) Photomicrograph of a specimen of Mesorbitolina texana showing the embryonic apparatus. Highstand normal regressive platforn carbonates of the Benassal Formation (early late Aptian). Depositional Sequence B. Scale = 1 mm. See Fig. 13 for location. B) Panoramic view of the lower uppe Aptian erosional subaerial unconformity incised into the highstand normal regressive platform top carbonates of the Benassal Formation. Note how the transgressiv surface is superposed onto the subaerial unconformity giving rise to a composite sequence boundary. This surface limits depositional sequences B and C. See Fig. 3 fo key and Figs. 12D and 13 for location. C) Close-up view of the sequence boundary between depositional sequences B and C exhibiting palaeokarst features, which ar found at the top of highstand normal regressive carbonates of the Benassal Formation. Note that the karst penetration depth is around 7 cm and how the sequenc boundary corresponds to an irregular erosional surface. Note also the presence of mud drapes. See Fig. 3 for key and Figs. 12D and 13 for location. D) Detail of th erosional subaerial unconformity exhibiting infilled palaeokarst features, which show a depth penetration of c. 9 cm. Note the presence of thin mud drapes. See Fig. | for key and Figs. 12D and 13 for location. E) Close-up view of the irregular subaerial unconformity overlain by thinly bedded strata belonging to transgressiv deposits of Depositional Sequence C. Note the presence of mud pebbles and of a lithoclast made up of highstand normal regressive platform top carbonates o Depositional Sequence B. Insect, and camera cap (= 5.8 cm) for scale. See Fig. 3 for key and Figs. 12D and 13 for location. F) Outcrop view of the composite sequenc boundary between the highstand platform top carbonates rich in Permocalculus and the higher-energy cross-bedded transgressive packstones and grainstones con taining abundant crinoid and Permocalculus debris. Hammer = 32 cm. See Fig. 3 for key and Figs. 12D and 13 for location.
Fig. 14. Loma de Camarillas. A) Photomicrograph of a specimen of Mesorbitolina texana showing the embryonic apparatus. Highstand normal regressive platforn carbonates of the Benassal Formation (early late Aptian). Depositional Sequence B. Scale = 1 mm. See Fig. 13 for location. B) Panoramic view of the lower uppe Aptian erosional subaerial unconformity incised into the highstand normal regressive platform top carbonates of the Benassal Formation. Note how the transgressiv surface is superposed onto the subaerial unconformity giving rise to a composite sequence boundary. This surface limits depositional sequences B and C. See Fig. 3 fo key and Figs. 12D and 13 for location. C) Close-up view of the sequence boundary between depositional sequences B and C exhibiting palaeokarst features, which ar found at the top of highstand normal regressive carbonates of the Benassal Formation. Note that the karst penetration depth is around 7 cm and how the sequenc boundary corresponds to an irregular erosional surface. Note also the presence of mud drapes. See Fig. 3 for key and Figs. 12D and 13 for location. D) Detail of th erosional subaerial unconformity exhibiting infilled palaeokarst features, which show a depth penetration of c. 9 cm. Note the presence of thin mud drapes. See Fig. | for key and Figs. 12D and 13 for location. E) Close-up view of the irregular subaerial unconformity overlain by thinly bedded strata belonging to transgressiv deposits of Depositional Sequence C. Note the presence of mud pebbles and of a lithoclast made up of highstand normal regressive platform top carbonates o Depositional Sequence B. Insect, and camera cap (= 5.8 cm) for scale. See Fig. 3 for key and Figs. 12D and 13 for location. F) Outcrop view of the composite sequenc boundary between the highstand platform top carbonates rich in Permocalculus and the higher-energy cross-bedded transgressive packstones and grainstones con taining abundant crinoid and Permocalculus debris. Hammer = 32 cm. See Fig. 3 for key and Figs. 12D and 13 for location.
Fig. 15. La Mola d’en Camaras. A) Panoramic view of the lower upper Aptian disconformity cropping out in the south-western face of the La Mola d’en Camaras in the Morella Sub-basin (see Bover-Arnal et al., 2014). B) Sequence-stratigraphic interpretation of Fig. 15A. Note the stepped nature of the deeply incised unconformity surface down-cutting at least 115 m into the underlying Aptian record. See also key in Fig. 3.
Fig. 15. La Mola d’en Camaras. A) Panoramic view of the lower upper Aptian disconformity cropping out in the south-western face of the La Mola d’en Camaras in the Morella Sub-basin (see Bover-Arnal et al., 2014). B) Sequence-stratigraphic interpretation of Fig. 15A. Note the stepped nature of the deeply incised unconformity surface down-cutting at least 115 m into the underlying Aptian record. See also key in Fig. 3.
Fig. 17. Locations with geological evidence for major relative sea-level falls and rises during the early Aptian (including the early/late Aptian boundary) and the late Aptian. Where reported, estimates of the amplitude of sea-level change are indicated. The occurrence of roughly coeval Aptian major sea-level falls and rises in different tectonic plates, including the records of incised valleys in Iberia, Eurasia, Arabia and North America, is strong evidence for major eustatic fluctuations during the Aptian Stage. The data from the different locations are taken from ‘this study; *Bover-Arnal et al. (2009, 2015, 2016); 3Schlagintweit et al. (2016); 4Fermdndez-Mendiola et al. (2013); Hfaiedh et al. (2013); ®Mehrabi et al. (2018); 7Wilmsen et al. (2015); Yilmaz and Altiner (2006); °Ruberti et al. (2013); 10Graziano and Raspini (2015, 2018); Musinec et al. (2012); 12, datte et al. (2005) and Pictet et al. (2015); 13R6hl and Ogg (1998); Mc ahagian et al. (1996), Zorina and Ruban (2012) and Zorina (2014, 2016); 18yan Buchem et al. (2018); 16yan Buchem et al. (2002, 2010), Hillgartner et al. (2003), Maurer et al. (2010, 2013), Raven et al. (2010), Yose et al. (2010) and Rameil et al. (2012); ?7Horner et al. (2019); *8Bover-Arnal et al. (2014, 2016); !°Hfaiedh et al. (2013), Ben Chaabane et al. (2021); ?°Graziano et al. (2016); 74Adatte et al. (2005); ?2Sahagian et al. (1996); 7?Medvedev et al. (2011).
Fig. 17. Locations with geological evidence for major relative sea-level falls and rises during the early Aptian (including the early/late Aptian boundary) and the late Aptian. Where reported, estimates of the amplitude of sea-level change are indicated. The occurrence of roughly coeval Aptian major sea-level falls and rises in different tectonic plates, including the records of incised valleys in Iberia, Eurasia, Arabia and North America, is strong evidence for major eustatic fluctuations during the Aptian Stage. The data from the different locations are taken from ‘this study; *Bover-Arnal et al. (2009, 2015, 2016); 3Schlagintweit et al. (2016); 4Fermdndez-Mendiola et al. (2013); Hfaiedh et al. (2013); ®Mehrabi et al. (2018); 7Wilmsen et al. (2015); Yilmaz and Altiner (2006); °Ruberti et al. (2013); 10Graziano and Raspini (2015, 2018); Musinec et al. (2012); 12, datte et al. (2005) and Pictet et al. (2015); 13R6hl and Ogg (1998); Mc ahagian et al. (1996), Zorina and Ruban (2012) and Zorina (2014, 2016); 18yan Buchem et al. (2018); 16yan Buchem et al. (2002, 2010), Hillgartner et al. (2003), Maurer et al. (2010, 2013), Raven et al. (2010), Yose et al. (2010) and Rameil et al. (2012); ?7Horner et al. (2019); *8Bover-Arnal et al. (2014, 2016); !°Hfaiedh et al. (2013), Ben Chaabane et al. (2021); ?°Graziano et al. (2016); 74Adatte et al. (2005); ?2Sahagian et al. (1996); 7?Medvedev et al. (2011).
sonin, A., Pucéat, E., Vennin, E., Mattioli, E., Aurell, M., Joachimiski, M., Barbarin, N., Laffont, R., 2016. Cool episode and platform demise in the Early Aptian: New insights on the links between climate and carbonate production. Paleoceanography 31, 66-80. https://doi.org/10.1002/2015PA002835.
sonin, A., Pucéat, E., Vennin, E., Mattioli, E., Aurell, M., Joachimiski, M., Barbarin, N., Laffont, R., 2016. Cool episode and platform demise in the Early Aptian: New insights on the links between climate and carbonate production. Paleoceanography 31, 66-80. https://doi.org/10.1002/2015PA002835.
Related topics:
Sequence StratigraphyCarbonate PlatformSea Level ChangesIncised valleyMaestrat Basin
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