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Fig. 17. Sequence Boundary 2 and dolomitized peritidal deposits of the Mola de la Saranyana. (A) Outcrop-scale view of the upper part of the preserved transgressive deposits of Depositional Sequence C banked against the incised highstand platform carbonates of Depositional Sequence B. South-western face of the Mola d’en Camaras See Fig. 3 for key. Geologist at upper left for scale is ca 1-8 m tall. (B) Detail of the Sequence Boundary 2 dis played in (A). Note the iron staining exhibited by the surface. White arrows point to encrusting oyster shells which are associated with marine onlap after subaerial exposure and, thus, indicate the superposition of a maxi mum regressive surface onto the subaerial unconformity. Camera cap = 5-8 cm. (C) Close-up view of the Sequence Boundary 2 shown in (A). Note the truncated external coral moulds and whitish and yellowish infillings (rec urow) exhibited by this composite surface. Visible part of pen = 5-7 cm. (D) Outcrop view of the well-beddec peritidal dolostones. Mola de la Saranyana. Hammer length = 32 cm.

Figure 17 Sequence Boundary 2 and dolomitized peritidal deposits of the Mola de la Saranyana. (A) Outcrop-scale view of the upper part of the preserved transgressive deposits of Depositional Sequence C banked against the incised highstand platform carbonates of Depositional Sequence B. South-western face of the Mola d’en Camaras See Fig. 3 for key. Geologist at upper left for scale is ca 1-8 m tall. (B) Detail of the Sequence Boundary 2 dis played in (A). Note the iron staining exhibited by the surface. White arrows point to encrusting oyster shells which are associated with marine onlap after subaerial exposure and, thus, indicate the superposition of a maxi mum regressive surface onto the subaerial unconformity. Camera cap = 5-8 cm. (C) Close-up view of the Sequence Boundary 2 shown in (A). Note the truncated external coral moulds and whitish and yellowish infillings (rec urow) exhibited by this composite surface. Visible part of pen = 5-7 cm. (D) Outcrop view of the well-beddec peritidal dolostones. Mola de la Saranyana. Hammer length = 32 cm.

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Fig. 1. (A) Geographical setting of the study area in the eastern Iberian Chain (East Iberian Peninsula). (B) Simpli- fied palaeogeographic and structural map of the Maestrat Basin during the Late Jurassic—Early Cretaceous rifting cycle and location of the study area in the Morella Sub-basin. Mo, Morella Sub-basin; Pe, El Perell6 Sub-basin; Sa, La Salzedella Sub-basin; Ga, Galve Sub-basin; Ol, Oliete Sub-basin; Al, Aliaga Sub-basin; Pg, Penyagolosa Sub-basin. Modified after Salas et al. (2001). (C) Geological setting of the studied hillocks. Modified after Navarro- Vazquez et al. (1972) and Martin et al. (1972).
Fig. 1. (A) Geographical setting of the study area in the eastern Iberian Chain (East Iberian Peninsula). (B) Simpli- fied palaeogeographic and structural map of the Maestrat Basin during the Late Jurassic—Early Cretaceous rifting cycle and location of the study area in the Morella Sub-basin. Mo, Morella Sub-basin; Pe, El Perell6 Sub-basin; Sa, La Salzedella Sub-basin; Ga, Galve Sub-basin; Ol, Oliete Sub-basin; Al, Aliaga Sub-basin; Pg, Penyagolosa Sub-basin. Modified after Salas et al. (2001). (C) Geological setting of the studied hillocks. Modified after Navarro- Vazquez et al. (1972) and Martin et al. (1972).
Fig. 2. Stratigraphic framework and age relations for the Aptian in the Morella Sub-basin. Local ranges of age- diagnostic fossils recognized are indicated. Identified ammonite biozones are taken from Moreno-Bedmar et al (2010). Absolute ages are from Gradstein et al. (2004).
Fig. 2. Stratigraphic framework and age relations for the Aptian in the Morella Sub-basin. Local ranges of age- diagnostic fossils recognized are indicated. Identified ammonite biozones are taken from Moreno-Bedmar et al (2010). Absolute ages are from Gradstein et al. (2004).
© 2014 The Authors. Sedimentology © 2014 International Association of Sedimentologists, Sedimentology
© 2014 The Authors. Sedimentology © 2014 International Association of Sedimentologists, Sedimentology
Fig. 4. Aerial photograph of the Mola d’en Camaras, Mola de la Vila, Mola de la Saranyana and Mola de la Garumba that surround the village of El Forcall. The location of the outcrops and lithofacies shown in Figs 5, 6, 8, 9, 10, 11B, 12B to G, 13 to 17 and 19 is indicated. Source of aerial photograph: SIGPAC photographs of the Spanish Ministry of Agriculture, Food and Environment.
Fig. 4. Aerial photograph of the Mola d’en Camaras, Mola de la Vila, Mola de la Saranyana and Mola de la Garumba that surround the village of El Forcall. The location of the outcrops and lithofacies shown in Figs 5, 6, 8, 9, 10, 11B, 12B to G, 13 to 17 and 19 is indicated. Source of aerial photograph: SIGPAC photographs of the Spanish Ministry of Agriculture, Food and Environment.
Fig. 5. Platform, slope, basin and platform-detached wedge lithofacies associations. (A) Detail of a floatstone tex ture containing small requieniid rudists and monopleurids. Highstand platform of Depositional Sequence B Benassal Formation, Late Aptian, Mola de la Garumba. Visible part of pen = 12-2 cm. (B) Detail of wholly preserved platy corals in growth position embedded in nodular marly limestones in slope settings. Lowstanc platform of Depositional Sequence B, Villarroya de los Pinares Formation, Early Aptian, Mola de la Garumba Hammer length = 32 cm. (C) Close-up view of two specimens of Plicatula placunea (centre), of an unidentifiec large bivalve (bottom centre) and of a small Deshayesites deshayesi specimen, which is indicated by the key Transgressive basinal marls of Depositional Sequence A, Forcall Formation, Early Aptian, Mola d’en Camaras. Vis ible part of key = 4-6 cm. (D) Photomicrograph of a moderately sorted grainstone texture with abundant peloid: and fragments of echinoids. Note the presence of a fragment of a bryozoan colony (centre right). The microfacie: is collected from the level with trough cross-bedding shown in Fig. 11B. Forced regressive unit of Depositiona Sequence A, Villarroya de los Pinares Formation, Early Aptian, Mola de la Garumba.
Fig. 5. Platform, slope, basin and platform-detached wedge lithofacies associations. (A) Detail of a floatstone tex ture containing small requieniid rudists and monopleurids. Highstand platform of Depositional Sequence B Benassal Formation, Late Aptian, Mola de la Garumba. Visible part of pen = 12-2 cm. (B) Detail of wholly preserved platy corals in growth position embedded in nodular marly limestones in slope settings. Lowstanc platform of Depositional Sequence B, Villarroya de los Pinares Formation, Early Aptian, Mola de la Garumba Hammer length = 32 cm. (C) Close-up view of two specimens of Plicatula placunea (centre), of an unidentifiec large bivalve (bottom centre) and of a small Deshayesites deshayesi specimen, which is indicated by the key Transgressive basinal marls of Depositional Sequence A, Forcall Formation, Early Aptian, Mola d’en Camaras. Vis ible part of key = 4-6 cm. (D) Photomicrograph of a moderately sorted grainstone texture with abundant peloid: and fragments of echinoids. Note the presence of a fragment of a bryozoan colony (centre right). The microfacie: is collected from the level with trough cross-bedding shown in Fig. 11B. Forced regressive unit of Depositiona Sequence A, Villarroya de los Pinares Formation, Early Aptian, Mola de la Garumba.
Fig. 7. Schematic block diagram showing the situation of the preserved sedimentary successions corresponding to the five hillocks studied (Mola de Morella, Mola d’en Camaras, Mola de la Saranyana, Mola de la Vila and Mola de la Garumba) within the conceptual model provided in Fig. 3. See Fig. 3 for key. intervals of white marls, decimetre-thick ochre nodular marly limestones and centimetre-thick to metre-thick limestones. Scattered oyster spec- imens are occasionally embedded within the marls. In the marly limestones, oysters are abundant and frequently display a clustered growth. Rarely, scleractinian colonies in growth position occur. The limestones exhibit different extures and bedding patterns. These comprise: i) white nodular mudstones, which occasion- ally display Thalassinoides, and contain scat- ered biseriate foraminifera, miliolids and fragments of echinoids; (ii) light grey, occasio- nally burrowed, wackestone to packstone tex- tures with peloids, orbitolinids, other foraminifera, and fragments of serpulids, gym- nocodiacean algae, echinoids, oysters and other molluscs; (iii) light grey and ochre floatstone to rudstone textures dominated by fragments of oysters, but also including rudist shells, fragments of other molluscs and echinoids, ben- thic foraminifera, peloids, unidentified burrows, ithoclasts (Fig. 6A) and mud pebbles and mud drapes (Fig. 6B); and (iv) ochre and light grey poorly sorted to well-sorted grainstones Fig. 6C), which exhibit cross-bedding, herring- bone cross-stratification (Fig. 6D), tidal bundles Fig. 6E) and burrows, and contain abundant peloids, miliolids, orbitolinids, other benthic foraminifera and fragments of echinoids, decapods, algae, bryozoans, oysters, gastropods and other molluscs. The grainstones with The Aptian record of the northern Maestrat Basin is subdivided into three depositional sequences (A, B and C) based on the distribu- tion of lithofacies, architecture of the strata and the identification of sequence stratigraphic surfaces. A 2D continuous platform to basin conceptual profile displaying the sedimentary response for each depositional sequence of the long-term relative sea-level evolution is pro- vided in Fig. 3. Figure 7 displays the position of each hillock (‘Mola’) studied within this conceptual model. A representative schematic log of the Mola de la Vila showing the vertical lithofacies evolution, the stratigraphic position
Fig. 7. Schematic block diagram showing the situation of the preserved sedimentary successions corresponding to the five hillocks studied (Mola de Morella, Mola d’en Camaras, Mola de la Saranyana, Mola de la Vila and Mola de la Garumba) within the conceptual model provided in Fig. 3. See Fig. 3 for key. intervals of white marls, decimetre-thick ochre nodular marly limestones and centimetre-thick to metre-thick limestones. Scattered oyster spec- imens are occasionally embedded within the marls. In the marly limestones, oysters are abundant and frequently display a clustered growth. Rarely, scleractinian colonies in growth position occur. The limestones exhibit different extures and bedding patterns. These comprise: i) white nodular mudstones, which occasion- ally display Thalassinoides, and contain scat- ered biseriate foraminifera, miliolids and fragments of echinoids; (ii) light grey, occasio- nally burrowed, wackestone to packstone tex- tures with peloids, orbitolinids, other foraminifera, and fragments of serpulids, gym- nocodiacean algae, echinoids, oysters and other molluscs; (iii) light grey and ochre floatstone to rudstone textures dominated by fragments of oysters, but also including rudist shells, fragments of other molluscs and echinoids, ben- thic foraminifera, peloids, unidentified burrows, ithoclasts (Fig. 6A) and mud pebbles and mud drapes (Fig. 6B); and (iv) ochre and light grey poorly sorted to well-sorted grainstones Fig. 6C), which exhibit cross-bedding, herring- bone cross-stratification (Fig. 6D), tidal bundles Fig. 6E) and burrows, and contain abundant peloids, miliolids, orbitolinids, other benthic foraminifera and fragments of echinoids, decapods, algae, bryozoans, oysters, gastropods and other molluscs. The grainstones with The Aptian record of the northern Maestrat Basin is subdivided into three depositional sequences (A, B and C) based on the distribu- tion of lithofacies, architecture of the strata and the identification of sequence stratigraphic surfaces. A 2D continuous platform to basin conceptual profile displaying the sedimentary response for each depositional sequence of the long-term relative sea-level evolution is pro- vided in Fig. 3. Figure 7 displays the position of each hillock (‘Mola’) studied within this conceptual model. A representative schematic log of the Mola de la Vila showing the vertical lithofacies evolution, the stratigraphic position
Fig. 9. Sequence stratigraphy. (A) Photomosaic of the north-eastern face of the Mola d’en Camaras. The area outlined in yellow corresponds to the close-up view provided in (B). Width of image is ca 2 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). Note how the lowstand platform (Villarroya de los Pinares Formation) of Depositional Sequence B is incised and onlapped by the transgressive deposits of Depositional Sequence C. See Fig. 3 for key. A close-up view of the area outlined in black is shown in Fig. 16.
Fig. 9. Sequence stratigraphy. (A) Photomosaic of the north-eastern face of the Mola d’en Camaras. The area outlined in yellow corresponds to the close-up view provided in (B). Width of image is ca 2 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). Note how the lowstand platform (Villarroya de los Pinares Formation) of Depositional Sequence B is incised and onlapped by the transgressive deposits of Depositional Sequence C. See Fig. 3 for key. A close-up view of the area outlined in black is shown in Fig. 16.
Fig. 10. Sequence stratigraphy. (A) Photomosaic of the north-western face of the Mola d’en Camaras. The areas out: lined in yellow and red correspond, respectively, to the close-up view provided in panel (B) and to the situation o: the highstand normal regressive platform of Depositional Sequence A shown in Fig. 11A. Width of image is cc 1-5 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). Note the significant thickness exhibited by the transgressive unit (marls of the Forcall Formation) of Depositional Sequence A. See Fig. 3 for key.
Fig. 10. Sequence stratigraphy. (A) Photomosaic of the north-western face of the Mola d’en Camaras. The areas out: lined in yellow and red correspond, respectively, to the close-up view provided in panel (B) and to the situation o: the highstand normal regressive platform of Depositional Sequence A shown in Fig. 11A. Width of image is cc 1-5 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). Note the significant thickness exhibited by the transgressive unit (marls of the Forcall Formation) of Depositional Sequence A. See Fig. 3 for key.
Fig. 11. Highstand normal regressive platform and forced regressive deposits of Depositional Sequence A (Villar- roya de los Pinares Formation). (A) Panoramic view of the town of Morella with its castle built on top of the pre- served highstand normal regressive platform carbonates of Depositional Sequence A. Width of image is ca 700 m. (B) Outcrop view of a platform-detached wedge showing trough cross-bedding. Forced regressive unit of Deposi- tional Sequence A, Villarroya de los Pinares Formation, Mola de la Garumba. Below the platform-detached wedge, highstand normal regressive marls of Depositional Sequence A (Forcall Formation, Early Aptian) are visible. The downlapping slopes of the lowstand normal regressive platform of Depositional Sequence B (Villarroya de los Pin- ares Formation, Early Aptian) are observable at the top of the image. See Fig. 3 for key. Hammer length = 32 cm.
Fig. 11. Highstand normal regressive platform and forced regressive deposits of Depositional Sequence A (Villar- roya de los Pinares Formation). (A) Panoramic view of the town of Morella with its castle built on top of the pre- served highstand normal regressive platform carbonates of Depositional Sequence A. Width of image is ca 700 m. (B) Outcrop view of a platform-detached wedge showing trough cross-bedding. Forced regressive unit of Deposi- tional Sequence A, Villarroya de los Pinares Formation, Mola de la Garumba. Below the platform-detached wedge, highstand normal regressive marls of Depositional Sequence A (Forcall Formation, Early Aptian) are visible. The downlapping slopes of the lowstand normal regressive platform of Depositional Sequence B (Villarroya de los Pin- ares Formation, Early Aptian) are observable at the top of the image. See Fig. 3 for key. Hammer length = 32 cm.
Fig. 12. Age-diagnostic fossils. (A) Detail of mutually attached caprinid rudists. Platform lithofacies associatio1 highstand normal regressive deposits of Depositional Sequence A, Villarroya de los Pinares Formation, Early Ay tian, Mola de Morella. Visible part of pen = 3-3 cm. (B) Close-up view of a section of a caprinid rudist (Caprin aff. parvula). Platform lithofacies association, lowstand normal regressive unit of Depositional Sequence B, Villa roya de los Pinares Formation, Early Aptian, Mola de la Garumba. Visible part of pen = 2-3 cm. (C) and (D) Dufrenoy: dufrenoyi, lateral and ventral views of the specimen PUAB (Coleccions de Paleontologia de la Universit Autonoma de Barcelona) 88390. Basin lithofacies association, transgressive deposits of Depositional Sequence | Benassal Formation, Early Aptian, Mola de la Vila. Scale bar: 1 cm. (E) Dufrenoyia dufrenoyi, lateral view of th specimen PUAB 88784. Basin lithofacies association, transgressive unit of Depositional Sequence B, Benassal Fo mation, Early Aptian, Mola de la Vila. Scale bar: 1 cm. (F) Orbitolinopsis simplex. Platform lithofacies associatio1 highstand normal regressive platform of Depositional Sequence B, Benassal Formation, Late Aptian, Mola de | Garumba. (G) Mesorbitolina texana. Platform lithofacies association, highstand deposits of Depositional Sequenc B, Benassal Formation, Late Aptian, Mola de la Garumba.
Fig. 12. Age-diagnostic fossils. (A) Detail of mutually attached caprinid rudists. Platform lithofacies associatio1 highstand normal regressive deposits of Depositional Sequence A, Villarroya de los Pinares Formation, Early Ay tian, Mola de Morella. Visible part of pen = 3-3 cm. (B) Close-up view of a section of a caprinid rudist (Caprin aff. parvula). Platform lithofacies association, lowstand normal regressive unit of Depositional Sequence B, Villa roya de los Pinares Formation, Early Aptian, Mola de la Garumba. Visible part of pen = 2-3 cm. (C) and (D) Dufrenoy: dufrenoyi, lateral and ventral views of the specimen PUAB (Coleccions de Paleontologia de la Universit Autonoma de Barcelona) 88390. Basin lithofacies association, transgressive deposits of Depositional Sequence | Benassal Formation, Early Aptian, Mola de la Vila. Scale bar: 1 cm. (E) Dufrenoyia dufrenoyi, lateral view of th specimen PUAB 88784. Basin lithofacies association, transgressive unit of Depositional Sequence B, Benassal Fo mation, Early Aptian, Mola de la Vila. Scale bar: 1 cm. (F) Orbitolinopsis simplex. Platform lithofacies associatio1 highstand normal regressive platform of Depositional Sequence B, Benassal Formation, Late Aptian, Mola de | Garumba. (G) Mesorbitolina texana. Platform lithofacies association, highstand deposits of Depositional Sequenc B, Benassal Formation, Late Aptian, Mola de la Garumba.
Fig. 13. Sequence stratigraphy. (A) Photomosaic of the north-eastern face of the Mola de la Garumba. The areé outlined in yellow corresponds to the close-up view displayed in (B). Width of image is ca 1-9 km. (B) Close-ur view of (A). (C) Sequence stratigraphic interpretation of (B). Note the channel-fill deposits exhibited by the low. stand platform at the Mola de la Garumba. The channel drained towards the north. Note also how the lowstanc platform of Depositional Sequence B passes laterally from platform to slope settings, and how these lowstanc slopes downlap over a forced regressive wedge of Depositional Sequence A. See Fig. 3 for key.
Fig. 13. Sequence stratigraphy. (A) Photomosaic of the north-eastern face of the Mola de la Garumba. The areé outlined in yellow corresponds to the close-up view displayed in (B). Width of image is ca 1-9 km. (B) Close-ur view of (A). (C) Sequence stratigraphic interpretation of (B). Note the channel-fill deposits exhibited by the low. stand platform at the Mola de la Garumba. The channel drained towards the north. Note also how the lowstanc platform of Depositional Sequence B passes laterally from platform to slope settings, and how these lowstanc slopes downlap over a forced regressive wedge of Depositional Sequence A. See Fig. 3 for key.
Fig. 14. Stratal geometries and drowning of the lowstand normal regressive platform of Depositional Sequence B. (A) Outcrop view of the south-western part of the Mola de la Garumba. Width of image is ca 50 m. (B) Sequence stratigraphic interpretation of (A). Note the prograding geometries displayed by the lowstand platform, and how the in situ platform lithofacies pass basinwards to slope settings. On top of the platform, the maximum regressive surface marks the drowning of the platform, which is buried by transgressive basin marls. (C) Close-up view of three oysters encrusting the maximum regressive surface, which exhibits an iron crust. Mola d’en Camaras. (D) Detail of the transgressive lag present in the Mola de la Garumba. Note how the transgressive lag drapes over an irregular maximum regressive surface. See Fig. 3 for key. Hammer length = 32 cm.
Fig. 14. Stratal geometries and drowning of the lowstand normal regressive platform of Depositional Sequence B. (A) Outcrop view of the south-western part of the Mola de la Garumba. Width of image is ca 50 m. (B) Sequence stratigraphic interpretation of (A). Note the prograding geometries displayed by the lowstand platform, and how the in situ platform lithofacies pass basinwards to slope settings. On top of the platform, the maximum regressive surface marks the drowning of the platform, which is buried by transgressive basin marls. (C) Close-up view of three oysters encrusting the maximum regressive surface, which exhibits an iron crust. Mola d’en Camaras. (D) Detail of the transgressive lag present in the Mola de la Garumba. Note how the transgressive lag drapes over an irregular maximum regressive surface. See Fig. 3 for key. Hammer length = 32 cm.
Fig. 15. Sequence stratigraphy. (A) Photomosaic of the south-western face of the Mola d’en Camaras. The area outlined in white corresponds to the close-up view displayed in (B). The area outlined in red is enlarged in Fig. 17A. Width of image is ca 3-3 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). In this image, the incision down-cuts the entire Depositional Sequence B. Note also the stepped shape (strath ter- races) displayed by the unconformable surface, which corresponds to Sequence Boundary 2, and how the trans- gressive strata of Depositional Sequence C onlap this surface. See Fig. 3 for key.
Fig. 15. Sequence stratigraphy. (A) Photomosaic of the south-western face of the Mola d’en Camaras. The area outlined in white corresponds to the close-up view displayed in (B). The area outlined in red is enlarged in Fig. 17A. Width of image is ca 3-3 km. (B) Close-up view of (A). (C) Sequence stratigraphic interpretation of (B). In this image, the incision down-cuts the entire Depositional Sequence B. Note also the stepped shape (strath ter- races) displayed by the unconformable surface, which corresponds to Sequence Boundary 2, and how the trans- gressive strata of Depositional Sequence C onlap this surface. See Fig. 3 for key.
Fig. 16. Sequence stratigraphy. (A) Close-up view of Fig. 9C. North-eastern face of the Mola d’en Camaras. Cliff is ca 50 m height. (B) Sequence stratigraphic interpretation of (A). In this view, the erosional surface cuts the Aptian deposits down to the lowstand carbonates of Depositional Sequence B. Note how the unconformable surface (Sequence Boundary 2) displays a stepped morphology (strath terraces) and how the transgressive deposits of Depositional Sequence C onlap this surface. See Fig. 3 for key.
Fig. 16. Sequence stratigraphy. (A) Close-up view of Fig. 9C. North-eastern face of the Mola d’en Camaras. Cliff is ca 50 m height. (B) Sequence stratigraphic interpretation of (A). In this view, the erosional surface cuts the Aptian deposits down to the lowstand carbonates of Depositional Sequence B. Note how the unconformable surface (Sequence Boundary 2) displays a stepped morphology (strath terraces) and how the transgressive deposits of Depositional Sequence C onlap this surface. See Fig. 3 for key.
Fig. 18. Incision characterization. (A) Geological map of the Mola d’en Camaras with the situation of the ero- sional surface. Elevation contours (grey lines) and the present maximum and minimum elevations of the incision on the NE and SW slopes are shown (black numbers). The contour line interval is 10 m. The black line marks the geological cross-section reconstructed in (B) and (C). See Figs 1C and 4 for location of the Mola d’en Camaras. (B) Geological cross-section of the seismic-scale incision present at the Mola d’en Camaras. The outcrop expression of the area marked with the segment is displayed in Fig. 19C and D. (C) Restoration to the pre-contractional stage (prior to the Alpine deformation) of the geological cross-section shown in (B). Note the kilometric-scale dimension (width) of the incision and the stepped nature (strath terraces) of the sides. The depth of the incised valley from the top of the highstand carbonates of Depositional Sequence B preserved to the bottom is 115 m. Assuming that the uppermost transgressive deposits of Depositional Sequence C preserved were sedimented within the incision, its maximum depth would then be 140 m.
Fig. 18. Incision characterization. (A) Geological map of the Mola d’en Camaras with the situation of the ero- sional surface. Elevation contours (grey lines) and the present maximum and minimum elevations of the incision on the NE and SW slopes are shown (black numbers). The contour line interval is 10 m. The black line marks the geological cross-section reconstructed in (B) and (C). See Figs 1C and 4 for location of the Mola d’en Camaras. (B) Geological cross-section of the seismic-scale incision present at the Mola d’en Camaras. The outcrop expression of the area marked with the segment is displayed in Fig. 19C and D. (C) Restoration to the pre-contractional stage (prior to the Alpine deformation) of the geological cross-section shown in (B). Note the kilometric-scale dimension (width) of the incision and the stepped nature (strath terraces) of the sides. The depth of the incised valley from the top of the highstand carbonates of Depositional Sequence B preserved to the bottom is 115 m. Assuming that the uppermost transgressive deposits of Depositional Sequence C preserved were sedimented within the incision, its maximum depth would then be 140 m.
Fig. 19. Incision characterization. (A) Panoramic view of the south-western face of the Mola d’en Camaras show. ing the Late Aptian incised valley documented. This photomosaic corresponds to the outcrop expression o: Fig. 18B. See Figs 1C and 4 for location of the Mola d’en Camaras. Width of image is ca 2-9 km. (B) Interpretatior of (A). The area outlined in yellow is enlarged in (C) and (D). (C) Outcrop expression of the area indicated with « segment in the geological cross-section displayed in Fig. 18B. (D) Interpretation of (C). See Fig. 18 for key.
Fig. 19. Incision characterization. (A) Panoramic view of the south-western face of the Mola d’en Camaras show. ing the Late Aptian incised valley documented. This photomosaic corresponds to the outcrop expression o: Fig. 18B. See Figs 1C and 4 for location of the Mola d’en Camaras. Width of image is ca 2-9 km. (B) Interpretatior of (A). The area outlined in yellow is enlarged in (C) and (D). (C) Outcrop expression of the area indicated with « segment in the geological cross-section displayed in Fig. 18B. (D) Interpretation of (C). See Fig. 18 for key.
Related topics:
PaleontologySequence StratigraphyIncised valleyCarbonate platformsSea-level Changes
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