Study of morpholithodynamics and modeling of coastal processes on Iturup island (Kuril islands)

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Abstract

Sediment redistribution on the beach and offshore slope are the main processes forming the accumulating marine terraces of Iturup Island. The intensity of these processes is controlled by tectonic and seismic activity associated with Kuril-Kamchatka subduction zone. The long-term changes of the island ground level are due to vertical tectonic movement, while the short-term changes are associated with seismicity. Studies of morpholithodynamic processes in the coastal zone on the island of Iturup were carried out using the methods of paleoseismology, geomorphological analysis, and computer modeling. Based on previously collected data, analysis of topographic maps and satellite imagery, and field measurements on Iturup Island in 2022–2023, digital maps and digital elevation models (DEMs) of the coastal zone of the Kuril Bay were constructed. Four buried scarps were discovered within the beach ridge sediments on the accumulative marine terrace, indicating vertical coseismic subsidence that periodically occurs on the Sea of Okhotsk coast of Iturup. Based on tephra from the Tarumae volcano, the approximate age of the young beach ridges has been established (about 280 years). Applied 3D modeling predicted the flooding of the territory at different sea levels. Coastal profile of equilibrium developed from the DEM using the Dean model indicated that the modern marine terrace is stable. The SBEACH software was used to simulated storm surges and storm frequencies at different sea level scenarios. It was concluded that the erosion of the accumulative marine terrace, where the city of Kurilsk is located is possible either by catastrophic storms of rare recurrence, or after abrupt coseismic subsidence of the coast, which can occur during a strong earthquake in the area of the southern segment of the Kuril-Kamchatka subduction zone.

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About the authors

A. L. Khomchanovsky

Institute of Volcanology and Seismology FEB RAS

Author for correspondence.
Email: khomscience@mail.ru
Russian Federation, Petropavlovsk-Kamchatsky

F. I. Batanov

Institute of Volcanology and Seismology FEB RAS

Email: khomscience@mail.ru
Russian Federation, Petropavlovsk-Kamchatsky

T. K. Pinegina

Institute of Volcanology and Seismology FEB RAS

Email: khomscience@mail.ru
Russian Federation, Petropavlovsk-Kamchatsky

O. R. Khubaeva

Institute of Volcanology and Seismology FEB RAS

Email: khomscience@mail.ru
Russian Federation, Petropavlovsk-Kamchatsky

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2. Fig. 1. Map of Kuril Bay (study area shown as shaded circle). 1 – water bodies; 2 – swamp; 3 – rivers; 4 – roads.

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3. Fig. 2. Bathymetric survey of the Kuril Bay (isobaths are drawn at 10 m intervals). 1 – depth measurement points (tacks); 2 – depth markers; 3 – isobaths.

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4. Fig. 3. Map of the marine accumulative terrace and shoreface of the Kuril Bay. 1 – measurement profiles; 2 – isobaths; 3 – rivers; 4 – roads; 5 – buried ledges; 6 – cliff; 7 – water bodies.

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5. Fig. 4. Coastal profiles (the sea shore on the left) and location of buried scarps (black lines – presumed position in the soil-pyroclastic sequence). (а) – location of the study area; (б) – location of profiles on the marine terrace; photo of scarps in Fig. 12, spatial location of scarps in Fig. 3.

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6. Fig. 5. Results of equilibrium beach profile simulation for the Kuril Bay. 1 – initial shoreface; 2 – theoretical equilibrium beach profile based on the Dean model.

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7. Fig. 6. Shoreface profiles of the Kuril Bay and linear trend (middle profile). 1 – the mouth of the Kurilka River; 2 – profile Б; 3 – profile B; 4 – medium profile.

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8. Fig. 7. Results of equilibrium beach profiles modeling for the Kuril Bay. Profiles: (а) – north-western profile (closest to the mouth of the Kurilka River), (б) – central profile, (в) – southeastern profile, (г)– equilibrium beach profile of the combined profile (location of profiles in Figs. 4 and 13). 1 – initial shoreface; 2 – theoretical equilibrium beach profiles based on Dean’s model.

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9. Fig. 8. Possible reshaping of the Kuril Bay coastal after a rise in relative sea level by 1 m as a result of hydrodynamic and geodynamic factors. 1 – initial profile; 2 – blurred section; 3 – road; 4 – initial sea level; 5 – sea level after lowering.

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10. Fig. 9. Inundation of the lower areas of Kurilsk at sea level rise of 1 m (yellow line) and 2 m (red line); shading in the figures on the right indicates the lowland near Lake Lebedinoe (1.5 km from the shore of the Sea of Okhotsk).

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11. Fig. 10. Reshape of profile 2 by a storm of 2% recurrence (172 h/year, H = 5 m). 1 – initial profile; 2 – storm of 2% recurrence, H = 5 m.

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12. Fig. 11. Reshape of profile 3 by different storms at different levels (enlarged scale of the foreshore zone). 1 – initial profile; 2 – extreme storm (H = 10 m, level +2 m); 3 – storm 2% recurrence (level +3 m).

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13. Fig. 12. Photo of buried scarps on the beach ridges of the Kuril Bay accumulative terrace and trench section of scarp “(а)” (coordinates: 45.22137, 147.8673). Scarps: (а) – second scarp, (б) – third scarp, (в) – first scarp; (г) – trench section of scarp “(а)”. Location of scarps in Figs. 3 and 4. 1 – compacted sea sand (cover of marine storm sediments); 2 – colluvial cone of outflow; 3 – layered pebble sediments of the riverbed; 4 – sediments of a shallow reservoir (seasonal floods); 5 – loamy horizon with light ash content (Ta-a?); 6 – layered sea sand.

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14. Fig. 13. General view of the accumulative terrace of the Kuril Bay with the location of measured profiles and buried scarps (numerals denote profiles of beach ridges (see Fig. 4), letters – profiles of the measured shoreface (see Figs. 6, 7).

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