Morphometry and elevation of the last interglacial tidal notches in tectonically stable coasts of the Mediterranean Sea

Antonioli, Fabrizio; Ferranti, Luigi; Stocchi, Paolo; Deiana, Giacomo; Presti, Valeria Lo; Furlani, Stefano; Marino, C.; Orrù, Paolo; Scicchitano, Giovanni; Trainito, Egidio; Anzidei, Marco; Bonamini, M.; Sansò, Paolo; Mastronuzzi, Giuseppe

doi:10.1016/j.earscirev.2018.06.017

Cited by 39 publications

(19 citation statements)

References 85 publications

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“…Similar movements, although of greater magnitude, have been found in the Gulf of Orosei and Capo Caccia [7].…”

Section: Olbia Gulf and Coastal Plainssupporting

confidence: 76%

“…Similar movements, although of greater magnitude, have been found in the Gulf of Orosei and Capo Caccia [7]. The sedimentary sequence of MIS 5.5 at Punta La Mandria has a lower thickness and rests discordantly on both Paleozoic granitoid substrate and Middle Jurassic arenaceous dolomitic limestone.…”

Section: Olbia Gulf and Coastal Plainssupporting

confidence: 65%

“…At 119 ka BP, the insolation was higher than today, the sea was about 8 m higher [7], but the CO 2 content in the atmosphere never exceeded 295 ppm. Meanwhile, today, with a lower insolation, but a much higher content of CO 2 , 415 ppm, we can also observe a sea level 8 m lower than 119 ka BP and a rise that exceeds the acceleration of 3 mm/year.…”

Section: Methodsmentioning

confidence: 91%

“…The sea level change along the Mediterranean coast is the sum of eustatic, glacio-hydro-isostatic and tectonic factors. The first is time dependent while the latter two also vary with location, and they consist to sum the different components of sea level rise in the following main steps: (a) the IPCC AR5 projections (RCP-8.5 upper limits scenarios reported in the IPCC 2019); (b) the long-term land vertical movements from geological data [7,8,16]; (c) the glacio-hydro-isostatic movement (GIA) [2]; (d) by combining eustatic, isostatic and tectonic data projected up to 2100, and 2300, we provided the expected sea levels at 2100 and 2300 for the investigated coastal areas and the expected inland extent of related marine flooding.…”

Section: Methodsmentioning

confidence: 99%

“…The objective of our w is to highlight at what altitude can the fossil signs of maximum marine ingression (fo and aged deposits) now be observed, which occurred during MIS 5.5 compared wit sea level projections for 2100 and 2300 (IPCC 2019) in the four coastal sites under s (Figure 1). We also take in consideration the MIS 5.5 maximum highstand comparin observed data in field with the ice model [7] projections for Sardinia and the Pontina P In addition, on the basis of the bathymetry and the available data and models, we tioned the 21.5 ka cal BP coastline reached during the LGM (last glacial maximum) o continental shelf in front of the Plains. Furthermore, on the basis of the IPCC projec we have calculated (adding the geological vertical movements) the altitude at which sea will be reached (according to the AR 8.5 scenario) at 2100 and 2300.…”

Section: Introductionmentioning

confidence: 99%

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MIS 5.5 Highstand and Future Sea Level Flooding at 2100 and 2300 in Tectonically Stable Areas of Central Mediterranean Sea: Sardinia and the Pontina Plain (Southern Latium), Italy

Deiana

Antonioli

Moretti

et al. 2021

Water

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Areas of the Mediterranean Sea are dynamic habitats in which human activities have been conducted for centuries and which feature micro-tidal environments with about 0.40 m of range. For this reason, human settlements are still concentrated along a narrow coastline strip, where any change in the sea level and coastal dynamics may impact anthropic activities. We analyzed light detection and ranging (LiDAR) and Copernicus Earth observation data. The aim of this research is to provide estimates and detailed maps (in three coastal plain of Sardinia (Italy) and in the Pontina Plain (southern Latium, Italy) of: (i) the past marine transgression occurred during MIS 5.5 highstand 119 kyrss BP; (ii) the coastline regression occurred during the last glacial maximum MIS 2 (21.5 krs cal BP); and (iii) the potential marine submersion for 2100 and 2300. The objective of this multidisciplinary study is to provide maps of sea level rise future scenarios using the IPCC RCP 8.5 2019 projections and glacio-hydro-isostatic movements for the above selected coastal zones (considered tectonically stable), which are the locations of touristic resorts, railways and heritage sites. We estimated a potential loss of land for the above areas of between about 146 km2 (IPCC 2019-RCP8.5 scenario) and 637 km2 along a coastline length of about 268 km.

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“…Similar movements, although of greater magnitude, have been found in the Gulf of Orosei and Capo Caccia [7].…”

Section: Olbia Gulf and Coastal Plainssupporting

confidence: 76%

Section: Olbia Gulf and Coastal Plainssupporting

confidence: 65%

Section: Methodsmentioning

confidence: 91%

Section: Methodsmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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MIS 5.5 Highstand and Future Sea Level Flooding at 2100 and 2300 in Tectonically Stable Areas of Central Mediterranean Sea: Sardinia and the Pontina Plain (Southern Latium), Italy

Deiana

Antonioli

Moretti

et al. 2021

Water

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Late Quaternary paleo sea level geomorphological markers of opposite vertical movements at Salina volcanic island (Aeolian Arc)

Lucchi

Ricchi

Romagnoli

et al. 2019

Earth Surf Processes Landf

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Raised marine terraces and submerged insular shelves are used through an integrated approach as markers of relative sea level changes along the flanks of the Salina volcanic island (Aeolian Arc, southern Italy) for the purpose of evaluating its crustal vertical deformation pattern through time. Paleo sea level positions are estimated for the terrace inner margins exposed subaerially at different elevations and the erosive shelf edges recognized offshore at different depths. Compared with the eustatic sea levels at the main highstands (for the terraces) and lowstands (for the shelf edges) derived from the literature, these paleo sea level markers allowed us to reconstruct the interplay among different processes shaping the flanks of the island and, in particular, to quantify the pattern, magnitudes and rates of vertical movements affecting the different sectors of Salina since the time of their formation. A uniform uplift process at rates of 0.35 m ka−1 during the Last Interglacial is estimated for Salina (extended to most of the Aeolian Arc) as evidence of a regional (tectonic) vertical deformation affecting the sub‐volcanic basement in a subduction‐related geodynamic context. Before that, a dominant subsidence at rates of 0.39–0.56 m ka−1 is instead suggested for the time interval between 465 ka (MIS 12) and the onset of the Last Interglacial (MIS 5.5, 124 ka). By matching the insular shelf edges with the main lowstands of the sea level curve, a relative age attribution is provided for the (mostly) submerged volcanic centres on which the deepest (and oldest) insular shelves were carved, with insights on the chronological development of the older stages of Salina and the early emergence of the island. The shift from subsidence to uplift at the Last Interglacial suggests a major geodynamic change and variation of the stress regime acting on the Aeolian sub‐volcanic basement. © 2019 John Wiley & Sons, Ltd.

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Two main highstands during the last interglacial: Insights from palaeoshorelines and marine terraced deposits along the Ionian coast of the Apulia region, southern Italy

De Santis,

Montagna,

Scicchitano

et al. 2024

Earth Surf Processes Landf

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Field data, U‐Th dating and amino acid racemisation (AAR) and epimerisation (IAE) analyses were performed in a sector of the Ionian coast of Apulia. Palaeoshoreline 1 (PS1) was identified at +40 ± 5 m with the associated terraced deposit 1 (TD1). Palaeoshoreline 2 (PS2) was identified at +30 ± 2 m with the associated terraced deposit 2 (TD2), characterised by five sub‐units. The sub‐units that mark the transgression have an age of 127.851 ± 1.47 ky BP (by U‐Th dating) and 128.4 ± 26.2 ky BP (by AAR); one of sub‐units marking the highstand falls within aminozone E (MIS 5.5) based on IAE. Palaeoshoreline 3 (PS3) was identified at +19 ± 2 m with the associated terraced deposit 3 (TD3); they mark the occurrence of a second, lower elevation MIS 5.5 highstand. TD3 dates back to aminozones E–D (MIS 5.5‐MIS 5.3) based on IAE and to 122.49 ± 1.25 ky BP by U‐Th dating. We considered two scenarios where the first highstand of MIS 5.5 occurred at 125 and 123 ky BP, with a sea level at +7.5 ± 1.5 m; we then calculated the uplift rate of PS2 for both scenarios: it resulted to be 0.18 ± 0.03 mm/year. These uplift rates were used to calculate the position of PS3 at 122.49 ± 1.25 (rounded to ⁓122 ky BP) as well as the position of the layer dated to 127.851 ± 1.47 ky BP (rounded to ⁓128 ky BP). The position of PS3 at the time of its formation (i.e., the sea level at ⁓122 ky BP, corresponding to the second highstand of MIS 5.5) was calculated to be −2.96 ± 5.42 m for Scenario 1 and −3.32 ± 5.47 m for Scenario 2. The sea level obtained by the layer dated to ~128 ky BP was found to have a value of −11.79 ± 6.29 m. Finally, we reconstructed a relative sea level (RSL) trend suggesting two main highstands during MIS 5.5, with the earlier higher than the second.

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Morphometry and elevation of the last interglacial tidal notches in tectonically stable coasts of the Mediterranean Sea

Cited by 39 publications

References 85 publications

MIS 5.5 Highstand and Future Sea Level Flooding at 2100 and 2300 in Tectonically Stable Areas of Central Mediterranean Sea: Sardinia and the Pontina Plain (Southern Latium), Italy

MIS 5.5 Highstand and Future Sea Level Flooding at 2100 and 2300 in Tectonically Stable Areas of Central Mediterranean Sea: Sardinia and the Pontina Plain (Southern Latium), Italy

Late Quaternary paleo sea level geomorphological markers of opposite vertical movements at Salina volcanic island (Aeolian Arc)

Two main highstands during the last interglacial: Insights from palaeoshorelines and marine terraced deposits along the Ionian coast of the Apulia region, southern Italy

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