Geophysical methods for the study of natural and human-induced changes in ground massifs of the permafrost zone

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Abstract

The article considers examples of experimental studies of natural and human-induced changes in the properties of cryolithozone with different lithology. Studies have shown that in order to control changes in the properties of an engineering geological section, geophysical monitoring of frozen rocks subject to degradation is of particular importance. An approach to the study of the state and properties of cryolithozone soils in situ is presented using the example of complex geophysical work at hydraulic engineering facilities in Western Yakutia, which helps us to understand the spatial and temporal patterns of the development of active thawed zones (taliks) over a relatively short time interval. Using the example of Bilibino NPP, built on permafrost, it is shown that the elastic properties of rocky frozen soils, usually fractured in the upper part of the section, depend not only on lithology, texture and structure, but also on the cryogenic state of rocks. The patterns of changes in the seismic properties of frozen hard rocks at this industrial site were analyzed as a result of the degradation of permafrost under the main structures associated with the heat release of reactor units for more than 30 years. It is shown that under the influence of the warming effect on the rocky frozen ground, the increment of seismic intensity can increase on average to +0.3 points relative to the surface of permafrost (initial conditions). The characteristics of seismic impacts (the values of PGA and the spectrum of the Samax reaction) change accordingly.

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About the authors

B. A. Trifonov

Sergeev Institute of Environmental Geoscience of the Russian Academy of Sciences

Author for correspondence.
Email: igelab@mail.ru
Russian Federation, Bldg. 2, 13, Ulansky All., Moscow, 101000

S. Yu. Milanovsky

Sergeev Institute of Environmental Geoscience of the Russian Academy of Sciences; Sсhmidt Institute of Physics of the Earth of the Russian Academy of Sciences

Email: svetmil@mail.ru
Russian Federation, Bldg. 2, 13, Ulansky All., Moscow, 101000; Bldg. 1, 10, B. Gruzinskaya St., Moscow, 123242

V. V. Nesynov

Sergeev Institute of Environmental Geoscience of the Russian Academy of Sciences

Email: igelab@mail.ru
Russian Federation, Bldg. 2, 13, Ulansky All., Moscow, 101000

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Supplementary files

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2. Fig. 1. Geological section (a), zero isotherms and dynamics of talik contour change (b), radarogram (c) along the Sytykanskaya dam axis, 1997-1998 [1].

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3. Fig. 2. Sytykansky hydroscheme: a - distribution of negative anomalies of natural electric field (EF) potential in the upper reservoir embankment; negative anomalies correspond to infiltration zones [1]; b - area control of bypass filtration in the melt zone of the right bank abutment according to joint interpretation of borehole thermometry and electrotomography data [2].

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4. Fig. 3. Examples of geoelectric sections: on the left - effective resistivity (ρ); on the right - relative permittivity (ε), along the profile of wells (4-5-6-7-10) in the frozen massif in the cross of the shoreline of the Sytykansky hydroelectric complex (Western Yakutia); ORVP observations: top - March 2001; middle - August 2001; bottom - March 2002. Frozen rocks are characterised by high ρ and low ε; thawed rocks are characterised by low ρ and high ε. The bottom level near the dam is 301 m [19, 26]. The horizontal axes show the distance from the shoreline and the vertical axes show the absolute depth marks, [m]. Translated with www.DeepL.com/Translator (free version)

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5. Fig. 4. Schematic location of the observation profile and piezometric (injection) well, right-bank abutment of the Sytykan reservoir, Western Yakutia (a). Regime (repeated) electrotomographic measurements to identify filtration windows and filtration rates. Filtration window at a depth of 25 m in the area of PK100m at 90 min after injection (b) [2].

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6. Fig. 5. Geoelectric sections based on RWGI results: 1999-2022 with gamma ray logging and electrical resistivity diagrams. Thermometry by wells for 1999, 2013 and 2022 is given [3].

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7. Fig. 6. Results of measuring microseismic signal amplitudes and soil temperature in borehole NB-5 in 2019 and 2022: 1 - bulk soil; 2 - dark grey dolerite, strong, strongly fractured, in some places destroyed to large rubble and clumps; 3 - interlayering of siltstones, sandstones and dolomite; 4 - dolomitised limestone, in some places destroyed to sandy loam with rubble and gravel [7].

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8. Fig. 7. Example of changes in the initial state of frozen rock soils along the section at the BWPP site during its operation since 1976. Graphs of temperature changes in well 8 (presumably summer, 1991), well 10 (presumably winter, 1991) and well 12 (regime measurements during 2012).

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9. Fig. 8. Examples of calculated accelerograms and corresponding response spectra Sa (5%) - 10-2 in fractions of g from the supposed local earthquake: M1 (model 1) - on the surface of frozen rock strata of the BWPP site (Amax = 9. 1 cm/s2); M2 (model 2) - on the surface of thawed rock strata at a total thaw depth of 35 m in 1991 (Amax = 10.0 cm/s2). 1 cm/s2); M2 (model 2) - on the surface of thawed rock strata at a total thaw depth of 35 m in 1991 (Amax = 10.0 cm/s2); M4 (model 4-predicted) - on the surface at a predicted total thaw depth of 65 m by 2023 (Amax = 12.0 cm/s2).

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