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) en The last interglacial in the Mediterranean as a model for the present interglacial
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| 93 | "name": "2768a10c-3337-5f0d-8127-1630e1d4471e", | 103 | "name": "2768a10c-3337-5f0d-8127-1630e1d4471e", | ||
| 94 | "notes": "Deposits of the Last Interglacial on the south and | 104 | "notes": "Deposits of the Last Interglacial on the south and | ||
| 95 | southeastern coasts of Spain are shallow marine and coastal sediments, | 105 | southeastern coasts of Spain are shallow marine and coastal sediments, | ||
| 96 | with a warm fauna of Strombus bubonius. These units exhibit a | 106 | with a warm fauna of Strombus bubonius. These units exhibit a | ||
| 97 | diversity of morpho-sedimentary models controlled by the tectonic | 107 | diversity of morpho-sedimentary models controlled by the tectonic | ||
| 98 | activity of the Mediterranean area, which is closely related to the | 108 | activity of the Mediterranean area, which is closely related to the | ||
| 99 | approximation of Africa and Iberia during the Quaternary.There are | 109 | approximation of Africa and Iberia during the Quaternary.There are | ||
| 100 | three well-dated peaks of maximum sea level (T-I: isotopic substage | 110 | three well-dated peaks of maximum sea level (T-I: isotopic substage | ||
| 101 | 7a, T-II: isotopic substage 5e, T-III: isotopic substage 5c). A | 111 | 7a, T-II: isotopic substage 5e, T-III: isotopic substage 5c). A | ||
| 102 | younger episode, T-IV, probably corresponds to the isotopic substage | 112 | younger episode, T-IV, probably corresponds to the isotopic substage | ||
| 103 | 5a. Episodes T-II, T-III and T-IV were laid down during Last | 113 | 5a. Episodes T-II, T-III and T-IV were laid down during Last | ||
| 104 | Interglacial age. In addition, three Holocene peaks of maximum sea | 114 | Interglacial age. In addition, three Holocene peaks of maximum sea | ||
| 105 | level: H-1 ca. 5100 yr B.P., H-2 ca. 3500 yr B.P. and H-3 ca. 2400 yr | 115 | level: H-1 ca. 5100 yr B.P., H-2 ca. 3500 yr B.P. and H-3 ca. 2400 yr | ||
| 106 | B.P. were found.The three main peaks of the Last Interglacial | 116 | B.P. were found.The three main peaks of the Last Interglacial | ||
| 107 | correspond to the morpho-sedimentary Tyrrhenian units T-II, T-III and | 117 | correspond to the morpho-sedimentary Tyrrhenian units T-II, T-III and | ||
| 108 | T-IV, deposited during a time span of some 45,000 years. Several | 118 | T-IV, deposited during a time span of some 45,000 years. Several | ||
| 109 | smaller oscillations can be distinguished within each of these units | 119 | smaller oscillations can be distinguished within each of these units | ||
| 110 | as subunits separated by erosional surfaces. At least three of such | 120 | as subunits separated by erosional surfaces. At least three of such | ||
| 111 | mapable subunits were distinguished within the peak T-II (5e); each | 121 | mapable subunits were distinguished within the peak T-II (5e); each | ||
| 112 | lasted ca. 10,500 yr.As the positive oscillations of sea level (H-1, | 122 | lasted ca. 10,500 yr.As the positive oscillations of sea level (H-1, | ||
| 113 | H-2, and H-3) recorded during the present Interglacial (Holocene) are | 123 | H-2, and H-3) recorded during the present Interglacial (Holocene) are | ||
| 114 | much shorter, we infer that they are smaller-scale fluctuations | 124 | much shorter, we infer that they are smaller-scale fluctuations | ||
| 115 | (2500-1100 yr cycles) within the first oscillation (duration: ca. | 125 | (2500-1100 yr cycles) within the first oscillation (duration: ca. | ||
| 116 | 10,500 yr) of the first Holocene peak of sea level which has not yet | 126 | 10,500 yr) of the first Holocene peak of sea level which has not yet | ||
| 117 | been completed.In addition to changes of sea level, the vertical and | 127 | been completed.In addition to changes of sea level, the vertical and | ||
| 118 | lateral arrangement of morpho-sedimentary units, which can be | 128 | lateral arrangement of morpho-sedimentary units, which can be | ||
| 119 | designated as the stratigraphic architecture, depends on tectonics and | 129 | designated as the stratigraphic architecture, depends on tectonics and | ||
| 120 | oceanography, including geoidal and steric changes and coastal | 130 | oceanography, including geoidal and steric changes and coastal | ||
| 121 | dynamics.The coastal dynamics factor largely depends on the exchange | 131 | dynamics.The coastal dynamics factor largely depends on the exchange | ||
| 122 | of waters between the Atlantic and the Mediterranean. Maximum | 132 | of waters between the Atlantic and the Mediterranean. Maximum | ||
| 123 | incursions of water coincides with warm periods (highstands) when the | 133 | incursions of water coincides with warm periods (highstands) when the | ||
| 124 | coastal accretion increases.The tectonic factor greatly influences and | 134 | coastal accretion increases.The tectonic factor greatly influences and | ||
| 125 | modifies the effects of sea-level changes in the coastal areas of | 135 | modifies the effects of sea-level changes in the coastal areas of | ||
| 126 | tectonically-active regions such as the Mediterranean. Areas with | 136 | tectonically-active regions such as the Mediterranean. Areas with | ||
| 127 | tectonic uplift will be characterized by a staircase of prograding | 137 | tectonic uplift will be characterized by a staircase of prograding | ||
| 128 | gravelly beaches, whereas sinking areas will favour the deposition of | 138 | gravelly beaches, whereas sinking areas will favour the deposition of | ||
| 129 | vertically stacked sequences with coastal onlap of barrier island and | 139 | vertically stacked sequences with coastal onlap of barrier island and | ||
| 130 | lagoon deposits.Rates of sea-level rise for the coming years of 1 | 140 | lagoon deposits.Rates of sea-level rise for the coming years of 1 | ||
| 131 | cm/yr, have been suggested by some authors. These gradients greatly | 141 | cm/yr, have been suggested by some authors. These gradients greatly | ||
| 132 | exceed those produced by any tectonic factor in the Spanish coast | 142 | exceed those produced by any tectonic factor in the Spanish coast | ||
| 133 | during the last 100 kyr. Shoreface erosion and transgression with | 143 | during the last 100 kyr. Shoreface erosion and transgression with | ||
| 134 | landward migration of barrier islands and lagoons will occur in | 144 | landward migration of barrier islands and lagoons will occur in | ||
| 135 | subsiding areas (Murcia-Alicante and Valencia), even with relatively | 145 | subsiding areas (Murcia-Alicante and Valencia), even with relatively | ||
| 136 | low rates of sea-level rise (less than 0.5 cm/yr). Higher rates of | 146 | low rates of sea-level rise (less than 0.5 cm/yr). Higher rates of | ||
| 137 | sea-level rise (0.5-1 cm/yr) will increase the transgressive trend. | 147 | sea-level rise (0.5-1 cm/yr) will increase the transgressive trend. | ||
| 138 | Areas with subsidence rates higher than 7.5 cm/kyr (Mar Menor and Oval | 148 | Areas with subsidence rates higher than 7.5 cm/kyr (Mar Menor and Oval | ||
| 139 | of Valencia) are prone to transgression and erosion of barrier islands | 149 | of Valencia) are prone to transgression and erosion of barrier islands | ||
| 140 | and lagoons both in the cases of stable and rising sea levels. Risks | 150 | and lagoons both in the cases of stable and rising sea levels. Risks | ||
| 141 | are smaller in areas with lower rates of subsidence (La Mata, Santa | 151 | are smaller in areas with lower rates of subsidence (La Mata, Santa | ||
| 142 | Pola and Torrevieja lagoons) when a stable sea level is considered; | 152 | Pola and Torrevieja lagoons) when a stable sea level is considered; | ||
| 143 | however, any rise of sea level will trigger coastal erosion.", | 153 | however, any rise of sea level will trigger coastal erosion.", | ||
| 144 | "notes_translated": { | 154 | "notes_translated": { | ||
| 145 | "es": "Deposits of the Last Interglacial on the south and | 155 | "es": "Deposits of the Last Interglacial on the south and | ||
| 146 | southeastern coasts of Spain are shallow marine and coastal sediments, | 156 | southeastern coasts of Spain are shallow marine and coastal sediments, | ||
| 147 | with a warm fauna of Strombus bubonius. These units exhibit a | 157 | with a warm fauna of Strombus bubonius. These units exhibit a | ||
| 148 | diversity of morpho-sedimentary models controlled by the tectonic | 158 | diversity of morpho-sedimentary models controlled by the tectonic | ||
| 149 | activity of the Mediterranean area, which is closely related to the | 159 | activity of the Mediterranean area, which is closely related to the | ||
| 150 | approximation of Africa and Iberia during the Quaternary.There are | 160 | approximation of Africa and Iberia during the Quaternary.There are | ||
| 151 | three well-dated peaks of maximum sea level (T-I: isotopic substage | 161 | three well-dated peaks of maximum sea level (T-I: isotopic substage | ||
| 152 | 7a, T-II: isotopic substage 5e, T-III: isotopic substage 5c). A | 162 | 7a, T-II: isotopic substage 5e, T-III: isotopic substage 5c). A | ||
| 153 | younger episode, T-IV, probably corresponds to the isotopic substage | 163 | younger episode, T-IV, probably corresponds to the isotopic substage | ||
| 154 | 5a. Episodes T-II, T-III and T-IV were laid down during Last | 164 | 5a. Episodes T-II, T-III and T-IV were laid down during Last | ||
| 155 | Interglacial age. In addition, three Holocene peaks of maximum sea | 165 | Interglacial age. In addition, three Holocene peaks of maximum sea | ||
| 156 | level: H-1 ca. 5100 yr B.P., H-2 ca. 3500 yr B.P. and H-3 ca. 2400 yr | 166 | level: H-1 ca. 5100 yr B.P., H-2 ca. 3500 yr B.P. and H-3 ca. 2400 yr | ||
| 157 | B.P. were found.The three main peaks of the Last Interglacial | 167 | B.P. were found.The three main peaks of the Last Interglacial | ||
| 158 | correspond to the morpho-sedimentary Tyrrhenian units T-II, T-III and | 168 | correspond to the morpho-sedimentary Tyrrhenian units T-II, T-III and | ||
| 159 | T-IV, deposited during a time span of some 45,000 years. Several | 169 | T-IV, deposited during a time span of some 45,000 years. Several | ||
| 160 | smaller oscillations can be distinguished within each of these units | 170 | smaller oscillations can be distinguished within each of these units | ||
| 161 | as subunits separated by erosional surfaces. At least three of such | 171 | as subunits separated by erosional surfaces. At least three of such | ||
| 162 | mapable subunits were distinguished within the peak T-II (5e); each | 172 | mapable subunits were distinguished within the peak T-II (5e); each | ||
| 163 | lasted ca. 10,500 yr.As the positive oscillations of sea level (H-1, | 173 | lasted ca. 10,500 yr.As the positive oscillations of sea level (H-1, | ||
| 164 | H-2, and H-3) recorded during the present Interglacial (Holocene) are | 174 | H-2, and H-3) recorded during the present Interglacial (Holocene) are | ||
| 165 | much shorter, we infer that they are smaller-scale fluctuations | 175 | much shorter, we infer that they are smaller-scale fluctuations | ||
| 166 | (2500-1100 yr cycles) within the first oscillation (duration: ca. | 176 | (2500-1100 yr cycles) within the first oscillation (duration: ca. | ||
| 167 | 10,500 yr) of the first Holocene peak of sea level which has not yet | 177 | 10,500 yr) of the first Holocene peak of sea level which has not yet | ||
| 168 | been completed.In addition to changes of sea level, the vertical and | 178 | been completed.In addition to changes of sea level, the vertical and | ||
| 169 | lateral arrangement of morpho-sedimentary units, which can be | 179 | lateral arrangement of morpho-sedimentary units, which can be | ||
| 170 | designated as the stratigraphic architecture, depends on tectonics and | 180 | designated as the stratigraphic architecture, depends on tectonics and | ||
| 171 | oceanography, including geoidal and steric changes and coastal | 181 | oceanography, including geoidal and steric changes and coastal | ||
| 172 | dynamics.The coastal dynamics factor largely depends on the exchange | 182 | dynamics.The coastal dynamics factor largely depends on the exchange | ||
| 173 | of waters between the Atlantic and the Mediterranean. Maximum | 183 | of waters between the Atlantic and the Mediterranean. Maximum | ||
| 174 | incursions of water coincides with warm periods (highstands) when the | 184 | incursions of water coincides with warm periods (highstands) when the | ||
| 175 | coastal accretion increases.The tectonic factor greatly influences and | 185 | coastal accretion increases.The tectonic factor greatly influences and | ||
| 176 | modifies the effects of sea-level changes in the coastal areas of | 186 | modifies the effects of sea-level changes in the coastal areas of | ||
| 177 | tectonically-active regions such as the Mediterranean. Areas with | 187 | tectonically-active regions such as the Mediterranean. Areas with | ||
| 178 | tectonic uplift will be characterized by a staircase of prograding | 188 | tectonic uplift will be characterized by a staircase of prograding | ||
| 179 | gravelly beaches, whereas sinking areas will favour the deposition of | 189 | gravelly beaches, whereas sinking areas will favour the deposition of | ||
| 180 | vertically stacked sequences with coastal onlap of barrier island and | 190 | vertically stacked sequences with coastal onlap of barrier island and | ||
| 181 | lagoon deposits.Rates of sea-level rise for the coming years of 1 | 191 | lagoon deposits.Rates of sea-level rise for the coming years of 1 | ||
| 182 | cm/yr, have been suggested by some authors. These gradients greatly | 192 | cm/yr, have been suggested by some authors. These gradients greatly | ||
| 183 | exceed those produced by any tectonic factor in the Spanish coast | 193 | exceed those produced by any tectonic factor in the Spanish coast | ||
| 184 | during the last 100 kyr. Shoreface erosion and transgression with | 194 | during the last 100 kyr. Shoreface erosion and transgression with | ||
| 185 | landward migration of barrier islands and lagoons will occur in | 195 | landward migration of barrier islands and lagoons will occur in | ||
| 186 | subsiding areas (Murcia-Alicante and Valencia), even with relatively | 196 | subsiding areas (Murcia-Alicante and Valencia), even with relatively | ||
| 187 | low rates of sea-level rise (less than 0.5 cm/yr). Higher rates of | 197 | low rates of sea-level rise (less than 0.5 cm/yr). Higher rates of | ||
| 188 | sea-level rise (0.5-1 cm/yr) will increase the transgressive trend. | 198 | sea-level rise (0.5-1 cm/yr) will increase the transgressive trend. | ||
| 189 | Areas with subsidence rates higher than 7.5 cm/kyr (Mar Menor and Oval | 199 | Areas with subsidence rates higher than 7.5 cm/kyr (Mar Menor and Oval | ||
| 190 | of Valencia) are prone to transgression and erosion of barrier islands | 200 | of Valencia) are prone to transgression and erosion of barrier islands | ||
| 191 | and lagoons both in the cases of stable and rising sea levels. Risks | 201 | and lagoons both in the cases of stable and rising sea levels. Risks | ||
| 192 | are smaller in areas with lower rates of subsidence (La Mata, Santa | 202 | are smaller in areas with lower rates of subsidence (La Mata, Santa | ||
| 193 | Pola and Torrevieja lagoons) when a stable sea level is considered; | 203 | Pola and Torrevieja lagoons) when a stable sea level is considered; | ||
| 194 | however, any rise of sea level will trigger coastal erosion." | 204 | however, any rise of sea level will trigger coastal erosion." | ||
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