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Sea-level Changes

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Sea-level changes refer to the variations in the height of the ocean's surface relative to land, influenced by factors such as climate change, glacial melting, thermal expansion of water, and tectonic activity. These changes can have significant impacts on coastal ecosystems, human settlements, and global climate patterns.
lightbulbAbout this topic
Sea-level changes refer to the variations in the height of the ocean's surface relative to land, influenced by factors such as climate change, glacial melting, thermal expansion of water, and tectonic activity. These changes can have significant impacts on coastal ecosystems, human settlements, and global climate patterns.
MPs to review UK's role in Arctic sustainability - 24th April 2017.docx
by Veli Albert Kallio

2017, House of Commons | Select Committee on Environmental Audit | UK's role in Arctic Sustainability Inquiry | ARC0003 | Written evidence from the Sea Research Society, Environmental Affairs Department | .docx file of the referenced text edition

The draft paper as at 24th April which is updated from the draft made for the oral presentation session (5th April 2017 does not contain any references and text errors needed corrections). The paper is still being worked on with more... more
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United Nations General Assembly Motion 101292 for UNFCCC's Talanoa Dialogue
by Veli Albert Kallio

2018, United Nations Framework Convention on Climate Change | UNFCCC 65045 | Talanoa Platform | The Bonn Conference

The United Nations Conference on Environment and Development (the Rio de Janeiro Earth Summit, UNCED), Rio de Janeiro, Brazil, held 3rd-14th June 1992, launched the United Nations Framework Convention on Climate Change (UNFCCC) which... more
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The Central Mediterranean
by Lucilla Capotondi
Central Mediterranean shelves show a large variability in morphology (width, slope, unevenness), stratigraphy (different thickness of depositional bodies resulting from the last climatic/eustatic cycle) and sedimentology (shelf-mud... more
Fig. 13.1 On the left, a digital elevation model of Italy and surrounding seas (data from www.gebco.net/); note the change from light blue to dark blue marks the approximate limit of the continental shelf. On the right, a simplified tectonic map of Italy and surrounding regions, modified from Scrocca et al. (2003) with permission. (1) foreland areas; (2) foredeep deposits (delimited by the -1000-m isobath); (3) domains characterized by a compressional tectonic regime in the Apennines; (4) thrust belt units accreted during the Alpine orogenesis; (5) areas affected by extensional tectonics in response to the eastward roll-back of the west-directed Apennine subduction; (6) outcrops of crystalline basement (including metamorphic alpine units); (7) regions characterized by oceanic crust; (8) Apennine watershed; (9) thrust; (10) faults. Fig. 13.1 On the left, a digital elevation model of Italy and surrounding seas (data from www.gebco.net/); note the change from light blue
Fig. 13.2 Map of the main tectono-stratigraphic units of Italy from the geological map of Italy at 1:1,250,000 scale (www.isprambiente.gov.it en/projects/soil-and-territory/the-geological-map-of-italy-1-250000-scale/default). Reproduced with permission from ISPRA.
Fig. 13.4 The bathymetric data used in this map were derived from GEBCO. Isobaths between -130m and -10 m are well defined in the Adriatic Sea.
Fig. 13.5 Close-up of Fig. 13.4 for the central Adriatic Sea.
Fig. 13.6 Close-up of Fig. 13.4 for the Tyrrhenian Sea.
Fig. 13.7 Rates of vertical movement along the Italian coastlines for MIS 5.5 (125 ka) and the Holocene. Modified from Lambeck et al. 2011
Fig. 13.8 Vertical displacement rates (mm/year) computed from the elevation of (A) Late Pleistocene and (B) Holocene markers plotted with main structures on a DEM of Calabria and eastern Sicily. Modified from Ferranti et al. 2010. Fig. 13.8 Vertical displacement rates (mm/year) computed from the elevation of (A) Late Pleistocene and (B) Holocene markers plotted wit
Fig. 13.11 DTM of the Panarea and Stromboli volcanoes. The DTMs are at 2.5-m and 5-m grid size at Panarea and Stromboli respectively. Local bathymetry in the area surrounding the Panarea archipelago (the islets of Panarelli, Dattilo, Lisca Nera, Bottaro, and Lisca Bianca) is at 0.5-m grid size, while regional bathymetry is at 10-m grid size.
Fig. 13.12 Plio-Quaternary sediment thickness around the Italian coasts (data from IBCM charts, adapted with permission), displaying three main depocenters (see text for detail). Fig. 13.12 Plio-Quaternary sediment thickness around the Italian coasts (data from IBCM charts, adapted with permission), displaying three
g. 13.13 (A) Thickness and depocenter distribution of the Late Holocene highstand mud-wedge in the Adriatic Sea. Modified from Cattan al. (2003) and reproduced with permission from Elsevier; on the right (B, C, D), thickness of highstand, transgressive and Quaternary posits. Data from 1:50.000 geological map of Italian sea ‘Venezia sheet’ (www.isprambiente.gov.it/ Media/carg/index_marine.html). 2produced with permission from ISPRA. Fig. 13.13 (A) Thickness and depocenter distribution of the Late Holocene highstand mud-wedge in the Adriatic Sea. Modified from Cattaneo
Fig. 13.14 Map of Holocene sediment thickness in the southern Latium shelf. Modified from Chiocci and La Monica (1996) with permission; note the main depocenters are located offshore of the main rivers draining this sector (the Tiber to the north and the Garigliano to the south). ocean. The hydrodynamics of the basin are controlled by the North Atlantic water inflow, wind regime, and climate of the surrounding lands (Pinardi & Masetti 2000). Climate variability is related to the geographic position of the region located on the transition between high- and low-latitude influences. Paleoceanographic research demonstrates that during the Last Glacial interval, the Mediterranean Sea became a sensitive region, respond- ing to North Atlantic rapid climatic changes, includ- ing Dansgaard-Oeschger (D-O) and Heinrich events (Rohling et al. 1998; Cacho et al. 1999; Sangiorgi et al. 2003; Sierro et al 2005). In addition, it seems that the African monsoon extended at certain times over the Mediterranean basin and has been responsible for an increase in precipitation leading to increased freshwater input, reduced deepwater ventilation and deposition of sapropel layers (Tzedakis 2007). Various efforts have been made to estimate Quaternary SSTs in the Mediterranean Sea but most of these studies have considered single- core rather than multi-core analysis on a basin-wide scale (Kallel et al. 1997; Sangiorgi et al. 2003; Geraga et al. 2005; Di Donato et al. 2008). Additional problems are related to the different adopted methods (e.g. size fraction of faunal counting, use of different proxies) and
Fig. 13.15 Mean April-May sea-surface temperatures (SST) during the LGM at 22 ka cal BP Figures are obtained by solving the
Fig. 13.16 Mean April-May sea-surface temperatures (SST) during the Holocene Climatic Optimum at 8 ka cal BP Figures are obtained by the same methods as for those presented in Fig. 13.15.
Fig. 13.17 Sardinia, Tyrrhenian Sea. DEM from GEBCO with
“ig. 13.18 Coast of southern Latium, Tyrrhenian Sea. DEM from
Fig. 13.20 Modified from Alvisi et al. (1994) and reproduced with permission from Istituto Italiano di Speleologia; black represents
Fig. 13.21 Alghero, Sardinia. A partially submerged cave containing
biased by selective pollen accumulation and preservation, resulting in an over-representation of the saccate pollen of conifers and in reduced floristic richness. The distance from the coast, and the water depth of the coring sites, clearly affect the vegetation reconstruction. The deep- sea records of the Adriatic Sea (-300m; Fig. 13.23) mostly represent the development of regional vegetation, as indicated by the high amounts of pollen from montane vegetation, corresponding to pollen inputs from far inland. In particular, both core KET 8216 and MD 90- 917 (Rossignol-Strick et al. 1992; Combourieu-Nebout et al. 1998) show significant percentages of Picea, most probably from the mountain ranges of the Balkan Peninsula. The vegetational landscape of the Italian coasts was herb-dominated, as also indicated by the coeval lacustrine records from inland regions (Follieri et al. 1998; Allen et al. 2000). Excluding Pinus, the most important trees were deciduous Quercus, which could populate areas both at middle elevations and along the coasts. By contrast, modest frequencies of evergreen Quercus were probably from low elevation sites. Marine cores from above 300 m depth in the Adriatic Sea, which were relatively close to the ancient coast, show high percentages of Juniperus, together with abundant steppe and grassland elements, while deciduous trees were less abundant than in the coeval deep-sea records (Lowe et al. 1996). Fig. 13.22 The Cala dell’Alabastro cave (San Felice Circeo, Italy, black line). The arrow indicates a Mesolithic site (Riparo Blanc) containing the shell mounds of limpets (Patella ferruginea) dated by radiocarbon; the submerged cave is of interest for future research. Modified from Antonioli and Ferranti (1994). Fig. 13.22 The Cala dell’Alabastro cave (San Felice Circeo, Italy, black line). The arrow indicates a Mesolithic site (Riparo Blanc) containing in the coeval deep-sea records (Lowe et al. 1996).
Fig. 13.23 Location of coastal and marine pollen records in Italy for the time interval 22 ka cal BP to 5ka cal BP (dot = land site; triangle Fig. 13.23 Location of coastal and marine pollen records in Italy for the time interval 22 ka cal BP to 5ka cal BP (dot = land site; triangle = marine site above 300 m; star = marine site below 300 m). The gray area represents the modern distribution of evergreen vegetation. (1) Mistras: Di Rita and Melis (2013); (2) Le Fango: Reille (1992); (3) Saleccia: Reille (1992); (4) Rapallo: Bellini et al. (2009); (5) Sestri Levante Bellini et al. (2009); (6) Lago di Massaciuccoli: Colombaroli et al. (2007); (7) Versilian Plain: Bellini et al. (2009); (8) Arno S1: Amorosi et al. (2009); (9) Pisa Plain: Bellini et al. (2009); (10) Arno M1: Aguzzi et al. (2007); (11) Ombrone: Biserni and van Geel (2005); (12) Lingua d’Oca-Interporto: Di Rita et al. (2010); (13) Pesce Luna: Milli et a/. (2013); (14) Vendicio: Aiello et al. (2007); (15) C106: Russo Ermolli and ¢ Pasquale (2002); Di Rita and Magri (2009); (16) KET 8003: Rossignol-Strick and Planchais (1989); (17) Lago Preola: Magny et al. (2011); (1: Gorgo Basso: Tinner et al. (2009); (19) Biviere di Gela: Noti et a/. (2009); (20) Burmarrad: Djamali et al. (2013); (21) Lago Alimini Piccolo: Di Rita and Magri (2009); (22) MD 90-917: Combourieu-Nebout et al. (1998); (23) KET 8216: Rossignol-Strick et al. (1992); (24) IN9: Zonnevelc (1996); (25) SAO3-1: Favaretto et al. (2008); (26) Lago Salso: Di Rita et al. (2011); Di Rita (2013); (27) Lago Battaglia: Caroli and Caldara (2007); Caldara et al. (2008); (28) RF93-30: Oldfield et al. (2003); (29) RF93-77: Lowe et al. (1996); (30) PAL94-8: Lowe et al. (1996); (31) CM92-43: Asioli et al. (2001); (32) Ca’ Fornera: Miola et al. (2010); (33) Concordia Sagittaria: Miola et al. (2010); (34) Lake Vrana: Schmidt et al. (2000); (35) Malo Jezero: Jahns and van den Bogaard (1998); (36) Lake Voulkaria: Jahns (2005); (37) Alikes Lagoon: Avramidis et al. (2012).
Fig. 13.24 Simplified map of the Italian continental shelf (in gray)
Fig. 13.25 The Grotta Verde (Sardinia, Italy) section of a Neolithic necropolis containing ceramics and skeletons at -9m and anthropic
Fig. 13.26 Emerged caves on land, on or close to the modern Fig. 13.26 Emerged caves on land, on or close to the modern coastline in northern Sicily containing prehistoric remains. Modified caves, some of which have been shown in recent studies to contain dated prehistoric sites, especially in central and southern Italy. At the moment the only prehistoric site that has published data is the Grotta Verde in northwest Sardinia (Alghero), containing Neolithic-age burials with Cardial pottery (6.7—7.2 ka cal BP, Antonioli et al. 1997 Fig. 13.25) and the site of Pakostane in Croatia (Radic Rossi & Antonioli 2008), where some hand-made wooden remains were found in situ at -5 m and dated to the Neolithic, although this research is still a work in progress. Finally, we illustrate some interesting caves (Fig. 13.26) located in northern Sicily close to the coast and above sea level containing prehistoric remains, while there are unstudied sea-flooded caves between —40 m and —15 m located in the surrounding cliffs. from Mannino and Thomas (2007) with permission from UCL.
In Sicily, the natural morpho-dynamic processes of the coastal sectors of Trapani and the Catania Plain have been compromised by land use and global changes. However, increasingly, erosion is affecting all the sandy beaches of the Italian littoral, where the dune systems have been strongly compromised or definitively destroyed. bathymetry_data/). This database provides a bathymetric grid at 30 arcsecond intervals, with reference to geograph- ical coordinates, latitude and longitude in the WGS84 datum. Bathymetry and topography were processed using the software Global Mapper 11 (www.globalmapper.com) in order to produce maps at different levels of detail (Fig. 13.5 and 13.6).
TABLE 13.2 PRINCIPAL RECONSTRUCTION OF SST PERFORMED IN THE CENTRAL MEDITERRANEAN SEA. Central Mediterranean wave climate reconstructions for the central Mediterranean Sea at different epochs. These predictions were then extended to the whole Mediterranean (Lambeck & Purcell 2005). A complete review of the Holocene data, including the files of the predicted sea-level data for 40 Italian sites, has recently been published (see supplementary material in Lambeck et a/. 2011). Significant differences can be observed in stable coastal areas if different sites are considered: as an example, sea level at 10 ka cal BP varies along the Italian coasts between —48 m and —35 m, whereas at about 8ka cal BP it ranges between -19m and —11 m. The Mesolithic and Neolithic paleoshorelines predicted from Lambeck et a/. (2011) for Sardinia and the central Mediterranean are drawn in Figs. 13.17 and 13.18, and other examples using the same method and model are published for the islands of Pianosa and Elba (Tuscany) in Antonioli e¢ a/. (2011). An example of temporal and spatial evolution of land/sea extension and paleoshoreline evolution since the LGM is reported in Furlani eg al. (2013) for the area between southern Sicily and northern Africa. The survival of prehistoric sites in shallow seas depends partly upon the prevailing local wave climate. Enclosed between the storm belt of northern Europe and the tropical area of northern Africa, the Mediterranean Sea has a relatively mild climate on average, but substantial storms are possible, usually in the six-month winter (Cavaleri et al. 1991). The maximum measured significant wave height (H,) can reach 10m, but model estimates for some non-documented storms suggest larger values. For instance, even in the relatively small Adriatic Sea, an oceanographic tower, located 15 km offshore in 16m water depth, suffered heavy damage up to 9 m above sea level (Cavaleri 2000).
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Bover-arnal et al 2014 (Sedimetology)
by ramon salas roig
Long-term relative sea-level cycles (0Á5 to 6 Myr) have yet to be fully understood for the Cretaceous. During the Aptian, in the northern Maestrat Basin (Eastern Iberian Peninsula), fault-controlled subsidence created depositional space,... more
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).
© 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. 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. 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. 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. 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. 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. 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.
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.
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Archaeological data as sea level proxies: Purported early and middle Holocene sea level stands (7-4 ka) in Alaska and Chukotka
by Owen Mason

2003, Final Conference Proceedings, IGCP 437, Otranto

Archaeological data can offer precision and extensive stratigraphic profiles, albeit restricted to discrete areas,
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Tidal notches: a sea-level indicator of uncertain archival trustworthiness
by Paolo P A Pirazzoli

2013, Palaegeography, Palaeoclimatology, Palaeoecology 369

After a short summary on the process and rates of intertidal bioerosion that deepens tidal notches, some case-studies are presented of tidal notches prevented from forming or being not preserved. In conclusion the lack of local fossil... more
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Sedimentary patterns and geometries of the Bahamian outer carbonate ramp (Miocene±Lower Pliocene, Great Bahama Bank
by John Reijmer
Core, logging and high-resolution seismic data from ODP Leg 166 were used to analyse deposits of the Neogene (Miocene±Lower Pliocene) Bahamian outer carbonate ramp. Ramp sediments are cyclic alternations of light-and dark-grey... more
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