The concentration of the main soluble ions in the ice wedges of IW-5 and IW-7 of the Batagay yedoma

Vasil'chuk Yurii Kirillovich ORCID: 0000-0001-5847-5568 Doctor of Geology and Mineralogy Professor, Lomonosov Moscow State University, Faculty of Geography, Department of Landscape Geochemistry and Soil Geography 119991, Russia, Moscow, Leninskie Gory str., 1, office 2009 vasilch_geo@mail.ru Other publications by this author

Introduction

The macronutrient composition of underground ice is formed by the combined influence of the ionic composition of the waters that formed these ices and the macrocomponent composition of the sediments containing the ice. For example, the underground ice in the kimberlite pipes of western Yakutia has a different ionic composition due to the fact that the rocks containing them contain significantly different amounts of anions and cations.^[1,2] The chemical composition of the formation ice of the Novosibirsk Islands generally reflects the macronutrient composition of their host sediments.^[3] Marine aerosols affect the salinization of the re-vein ice of Sibiryakova Island.^[4] The decrease in NaCl salinity of the Sibiryakov Island reflects the almost complete loss of the influence of the sea on the composition of ice in the Holocene.^[5]

The macronutrient composition can be used as an indicator of the change in geochemical conditions of migration and accumulation of chemical elements occurring as a result of the change in landscape conditions of ice formation. The total mineralization of the North Yakut ice is relatively low (up to 90 mg/l), however, salinity anomalies occur (from less than 30 mg/l to 400-430 mg/l).^[6,7]

Earlier, with the participation of the author, the ionic composition of other veins of the Batagai edoma was analyzed and some generalized information about the salinity of re-vein ice No. 17 and No. 20 was provided.^[8-10]

Geochemical composition of Late Pleistocene re-vein ice in the edom strata of the Stanchikov Yar and near the village. Chersky in the north of Yakutia was also studied using the same Steyer device as the veins of the Batagai section.^[11]

Iizuka et al.^[12] conducted a study of vein ice exposed by the Cape Barrow outcrop (Northern Alaska). Ca ²⁺, Na⁺, SO ₄ ^2-, NO ₃^-, Cl^- and other ions that make up the ice were of marine and continental origin. The ratio of concentrations of identical ions of marine and continental origin indicates the different role of seawater in the formation of the macronutrient composition of ice. The researchers found that the entire volume of Na⁺ is of marine origin. Ca ²⁺ and SO ₄ ^{2- ions were of continental origin}, contained in an amount of 0.022 mmol/l and 0.06 mmol/l, respectively. Thus, it was found that the macro-component composition of vein ice was formed under the combined influence of ice-containing soils (Ca ²⁺, SO ₄ ^2-) and waters of the Beaufort Sea (Na⁺, Cl^-, Br^-).

To. Campbell-Heaton^[13] the isotopic and ionic composition of Holocene and Late Pleistocene ice veins has been studied in re-vein ice in the territory of Eureka Sound and Mokka Fjord and in Nunavut. She found that ice veins of medium width (1-2 m) are better suited for paleoreconstructions, since these wedges retain a higher temporal resolution due to the high probability of cracking. With horizontal sampling of four ice veins, it was found that frost-breaking cracks do not always form in the center of the veins, new ice is formed quite randomly on both sides of the center. This was confirmed by radiocarbon measurements of the ice veins, showing an arbitrary age change from the center to the edge. Therefore, in order to establish the correct chronology of samples, it is necessary to rely on direct AMS dating of ice veins.^[13]

The purpose of this work is to study the composition of ions in the ice of re-vein ice No. 5 and No. 7 of the Batagai Edoma in order to determine the main source of ice formation.

Objects and methods

Batagai ravine

The authors studied syngenetic re-vein ice that opens up in the Batagai ravine (67°34'49" s.w., 134°46'19" v.d.), located 10 km south-east of the village. Batagai, in Verkhoyansk ulus, Republic of Yakutia (Sakha) (Fig. 1).

Fig. 1. Location of the Batagai crater (mega-ravine)

Fig. 2. Edoma in the eastern part of the outcrop of the Batagai crater

Batagaisky ravine (also called Batagaika due to its proximity to the Batagaika River) is located within the Yano-Adychsky plateau in the basin of the Yana River, it is surrounded by the Chersky Ridge in the east, the Verkhoyansky Ridge in the west and the Elginsky Plateau in the south. The Yano-Adych plateau is composed of siltstones, sandstones, clay shales of the Triassic and Jurassic, broken through by granite intrusions.

Batagai ravine is located on a slope facing southeast 1.5 km downhill at the foot of Mount Kirgilyakh, whose absolute height is 612 m. The length of the ravine in 2019 is 2.29 km, the width is 1 km, and the average depth is about 80 m. The western side of the ravine, located higher up the slope than the eastern one, has an absolute height of 325 m, and the eastern one is 38 m lower, its absolute height is 287 m, the average slope between the western and eastern sides is 4.7%. A review of a series of multisensory satellite images of the Batagai ravine from 1991 to 2018 showed that the area of the ravine increased at least 3 times – from 0.19 to 0.78 km2, the most significant increase occurred between 2010 and 2014, and then slowed down.^[14]

The absolute heights of the tested ice veins (PL or IW) and textured ice (TL): PL-5 – 273-266 m; PL-7 – 239-226 m. The points PZHL-5 and PZHL-7 belong to the eastern side of the ravine (Fig. 3).

Fig. 3. Location of the tested outcrops of the PZHL-5 and PZHL-7 re-vein ice. R. Were also tested. To compare their chemical composition with the chemical composition of veins: 1 – sampling points; 2 – ionic composition of ice; 3 – the content of basic elements in ice and soil inclusions in ice; 4 – the content of trace elements in ice and soil inclusions

Fig. 4. Section of the tested outcrop of PZHL-5 re-vein ice

Fig. 5. Section of the tested outcrop of PZHL-7 re-vein ice

Based on earlier studies^[15], including our own data^[16-18], we consider IW-5 and IW-7 as re-vein ices of the Late Pleistocene edom complex.

The climate, according to the Batagai weather station, is close to moderately cold.^[19] The average annual air temperature is -14.8 °C. The coldest month is January with temperatures from -43 to -51 °C.^[20] About 194 mm of precipitation falls per year. The driest months are March, January and February – usually no more than 5 mm of precipitation. Most of the precipitation falls here in July to 43 mm, with an average of 37 mm. The prevailing wind in winter (January) is south-westerly, in summer (July) – north or north-easterly.

Permafrost rocks in the basin of the The Yana have a continuous distribution. The active layer reaches a thickness of only 0.2-0.4 m under forest and moss, and 0.4-1.2 m in open areas. Permafrost rocks are highly acidic, cryogenic processes are widespread: thermokarst, thermal erosion, solifluction, weathering, frost cracking, etc.

Vegetation of the North taiga and forest-tundra type. Larch woodlands dominate. The species composition is represented by Kayander larch, birch, dwarf birch, alder, cedar elfin, bagulnik, Toll's foot, loose sedge, Siberian chicory, lingonberry, blueberry, moss-lichen complexes.^[21]

Compared with the soil cover of the western part of Yakutia, where, despite similar harsh climatic conditions, there are mainly permafrost analogues of subboreal soils (gray forest permafrost – under small–leaved vegetation on watersheds, permafrost – under coniferous forests, permafrost - on sloping surfaces), in the eastern part of Yakutia, the structure of the soil cover is represented by typical soils of boreal and forest-tundra zones.^[22]

Permafrost underdeveloped (primitive) rocky soils (regosols) are usually formed on mountain plateaus and their slopes, on stony or gravelly deposits under cedar-clade and rare-coniferous taiga vegetation.^[23] These soils represent only one low-power horizon with a low humus content, under which the soil-forming rock lies.^[24]

On the slopes, on the mountain-slope type of terrain, the above types of soils are gradually replaced by permafrost contours, which are formed on eluvial and eluvo-deluvial deposits under larch trees. These soils are widespread in the study area and occupy a significant part of this territory.

Permafrost peat and humus-gley soils have been formed on the hollows of the runoff, the bottoms of the valleys of small rivers (shallow valley types of terrain). They are usually distributed in local areas and occupy small areas. The floodplain landscapes of the Yana and Batagaika rivers are represented by permafrost alluvial layered underdeveloped (primitive) sandy soils and a variety of permafrost alluvial soils.^[24]

In the explanatory note to the state geological map^[25], the area of the village Batagai is designated as a rare metal-tungsten-tin ore region with reserves of such metals as: Cu, Zn, W, Pb, Sn, Zn, Li, Bi, Cd, Ga, Tl, Rb, Cs. Tin deposits near the villages of Batagai and Esse Khaya were actively developed earlier. In the 1990s, mining stopped. The formation of the ravine is associated with deforestation on the Kirgilyakh slope, as well as the development of tin deposits in the 1940s and 60s and further thermokarst erosion.^[24]

Sampling and sample preparation

Ice samples from the re-vein ice exposed by the exposure of the Batagai ravine were taken in August 2018.

Ice samples were taken from ice veins vertically every 10 cm using Makita DDF481rte 18B and Bosch GSR 36 VE-2-LI drills with steel ice crowns with a diameter of 51 mm.

Fig. 6. The sampling route using an electric drill (round holes) from the outcrop of re-vein ice of PZHL-7

To clean the sampling site, a near-surface layer with a thickness of 2-3 cm of ice was removed using a drill and further deeper samples were taken from the same hole. An ice sample with a diameter of 5 cm. it was drilled out of the veins, while the mass of each sample was about 150 g and packed in plastic bags. The ice selection was accompanied by a detailed description of the color, transparency, structure, thickness of ice and soil veins, inclusions, shape and size of xenoliths, and air bubbles. The coordinates of the sections were recorded using GPS.

Samples for ¹⁴ C dating were cut out of ice veins using an axe in such a way that the mass of each sample was at least 0.5-1 kg. The cut ice was packed in plastic bags (Fig. 7).

Fig. 7. Samples for ¹⁴ C dating cut out of the PZHL-7 ice vein using an axe

The ice was melted in bags at a temperature of +20 ° C. Each sample of thawed ice water was divided into 2 equal parts – filtered and unfiltered. "Unfiltered water" means that a sample of this water was poured into a vial immediately after thawing the ice without any additional manipulation. pH and EC meters were used to measure the acidity and electrical conductivity of melt water. The technical characteristics of the HANNA pHep 4 HI98127 pH meter are as follows: pH range - from 0.0–14.0; measurement accuracy – up to 0.1 pH units; measurement error – 0.1 pH units. The technical characteristics of the HANNA HI 98311 EC meter are as follows: the range of electrical conductivity is from 0.0 to 3999.0 µS/cm; the measurement accuracy is up to 0.1 µS/cm, the EC–TDS conversion coefficient is 0.45. Then the meltwater was poured into plastic bottles with a capacity of 10 ml with a tightly closed lid.

Laboratory analysis

Measurements of the macrocomponent composition of ice were carried out using the ion chromatograph "Steyer" (Russia), the detection limit for chloride ion is 0.02 mg/l. The ion chromatograph "Steyer" is designed for qualitative and quantitative determination of inorganic compounds F^-, Cl^-, NO ₃^-, NO ₂^-, SO ₄ ^2-, PO ₄ ^3-, Na⁺. NH ₄⁺, K⁺, Mg ²⁺ and Ca ²⁺ in aqueous solutions of various origins (natural, technical, drinking).

His device includes an isocratic pump, a conductometric detector, a separation column, a background conduction suppression system and a computer kit for collecting, processing and storing chromatographic data.

For samples from recycled ice, a method was used to measure the mass concentration of Ca ²⁺, Mg ²⁺, Na⁺, K⁺, NH ₄^{+ cations} in samples of drinking, mineral, natural and waste water by ion chromatography FR.1.31.2005.01738. The range of detectable concentrations is 0.10-20.00 mg/^dm3, and for the determination of anions, the method of measuring the mass concentration of Cl^-, SO ₄ ^2-, NO ₃^- in samples of drinking, mineral, natural and wastewater by ion chromatography FR.1.31.2005.01724 was used. The range of detectable concentrations is 0.10-20.00 mg/^dm3 and the method of measuring the mass concentration of ions in samples of natural, drinking and wastewater by ion chromatography HDPE F 14.1:2:4. 132-98. The range of detectable concentrations for cations is 0.10-150.00 mg/^dm3.

Using this method, the composition of melt water was measured in PL 5 and 7.

Results

Ionic composition of ice and macronutrient content

The ionic composition of the vein ice exposed in the Batagai ravine in 35 samples from PLL 5 and 36 samples from PLL 7 was studied.

Concentrations of macronutrients were determined for PGL-5 and PGL-7: K⁺, Na⁺, Ca ²⁺, Mg ²⁺, Cl^-, NO ₃^-, SO ₄ ^2-. The ice under study is mostly slightly alkaline. The minimum EU values of the Late Pleistocene re-vein ice of PZHL-5 in the Batagai edom are 72 µS/cm, the maximum 286 and average 133 µS/cm, and PZHL-7, 71, 296 and 121 msm, respectively, respectively, i.e. the total mineralization of PZHL-5 and PZHL-7 is very close. All ices are oxygen-based in terms of redox potential (Eh), that is, the conditions of migration of elements are oxidative and slightly alkaline. The PZHL ice is mainly fresh (the average amount of PZHL ions is 5,200 mg/l, (the average amount of PZHL ions is 7,164 mg/l) according to the PZHL classification.^[7] In PZHL-5, the maximum mineralization values reach 424 mg/l, which makes it possible to classify this ice sample as slightly salted.

In the dissolved form, Ca ²⁺ dominates among the studied PPL cations (PPL-5 from 17.8 to 82.5 mg/l, PPL-7 from 12.0 to 52.1 mg/l), Mg ²⁺ is in second place (PPL-5 from 3.1 to 13.6 mg/l, PPL-7 from 2.6 to 8.3 mg/l).

Na⁺ and K⁺ are contained in dissolved form in smaller amounts: Na⁺ – PL-5 from 0.8 to 6.8 mg / l, PL-7 from 0.45 to 4.0 mg / l, and K⁺ – PL-5 from 17.8 to 82.5 mg/l, PL-7 from 1.1 to 5.6 mg/l.

Nitrates (NO ₃^{-) prevail among the anions}: PLL-5 from 6.9 to 27.9 mg/l, PLL-7 from 5.0 to 54.8 mg/l, the average content of NO ₃^-: PLL-5 14.5 mg/l, PLL-7 12.2 mg/l (see Tables 1, 2).

Table 1. Ionic composition of Late Pleistocene re-vein ice, PZHL-5, Batagayskaya edoma

67°34ʹ 56ʹʹ s.w., 134°46ʹ 53ʹʹ v.d. (No.5-52) ice extraction from ch. 9.25-16.35 m ( 273.75 - 266.65 m abs. height)

Table 2. Ionic composition of Late Pleistocene re-vein ice, PZHL-7, Batagayskaya edoma

67°34ʹ 56ʹʹ s.w., 134°46ʹ 53ʹʹ v.d. (No.71-150) ice extraction from ch. 1-12.8 m (239-227.2 m abs. height)

The content of SO ₄ ^{2- and Cl}- ^anions. In the PHL-5 of the Batagai edoma, the content of SO ₄ ^2- varies from 2 to 17 mg/l, averaging 6.35 mg/l, the content of Cl^- varies from 1.08 to 7 mg/l, averaging 2.6 mg/l (Fig. 8). In the PHL-7 of the Batagai edoma, the content SO ₄ ^2- varies from 1.4 to 40.5 mg/l, averaging 6.35 mg/l (Fig. 9), the content of Cl^- varies from 1.13 to 4.5 mg/l, averaging 1.96 mg/l (see Tables 1, 2).

Fig. 8. Ionic composition of Late Pleistocene re-vein ice, PZHL-5, Batagayskaya edoma (67°34ʹ 56ʹʹ s.w., 134°46ʹ 53ʹʹ vd.)

Fig. 9. Ionic composition of Late Pleistocene re-vein ice, PZHL-7, Batagayskaya edoma (67°34ʹ 56ʹʹ s.w., 134°46ʹ 53ʹʹ vd.)

Discussion

Radiocarbon age of PGL-5 and PGL-7

Radiocarbon AMS dating performed by the authors directly from organic microinclusions from a number of PLL of the Batagai edoma demonstrated that the formation time of PLL-5 dates from the period from 48.1 to 44.9 thousand calibers. years ago, and PZHL-7 – from 48.9 to 46.2 thousand caliber. years ago.^[16-18]

Ionic composition

Previously studied by us^[11] by the same method, the PPL in the lower reaches of the Kolyma (village of Chersky) and the Mal river. Anyu (Stanchikov Yar) demonstrated slightly lower concentrations of sulfates (on average 1.2 - Chersky and 2.6 mg/l - Stanchikov) and chlorides (on average 1.8 - Chersky and 2.6 mg/l - Stanchikov)

In the pancreas of the Cherskaya edoma, the content of SO ₄ ² varies from 2.1 to 3.1 mg/l, averaging 2.6 mg/l; the content of Cl varies from 0.4 to 3.9 mg/l, averaging 1.2 mg/l.^[11]

The two adjacent ice veins PZHL-17 and PZHL-20 studied by us in the Batagai edom^[10] also belong to ultra-fresh ice with a concentration of basic ions from 20 to 40 mg/l. However, sodium and calcium cations significantly predominate in the ionic composition of the PZHL-17 re-vein ice, reaching 24.15 and 53.16 mg/l in one of the samples, respectively. In the same sample, chlorine anions reach 34.51 mg/l. The average concentration of sulfate anions is 2-3 mg/l. Sodium and calcium cations significantly predominate in the ionic composition of the PZHL-20 re-vein ice, reaching 7.27 and 50.0 mg/l, respectively, in one of the samples. In the same sample, chlorine anions reach 13.72 mg/l. The average concentration of sulfate anions is 2-4 mg/l, reaching 22.24 mg/l. The content of calcium cations is 6-20 mg/l (rarely reaching 42-53 mg/l); The concentration of potassium cations is 0.7-3 mg/l. The presence of nitrate anions in the composition of PZHL-17 is noticeable, amounting mainly to 4-7 mg/l at the extreme of NO ₃^-reaches 16 and even 26 mg/l at a depth of 12.5 m. In the composition of PZHL-20, nitrate anions are mainly 6-8 mg/l and reach a depth of 7-8 m - 13 mg/l.

According to K. Campbell-Heaton^[13], in the territory of Eureka Sound and Mokka Fjord (Fig. 10) in the EU18-W1 section: the content of SO ₄ ² varies from 46 to 127 mg/l, the content of Cl varies from 14 to 71 mg/l; in the EU18-W2 section: the content of SO ₄ ² varies from 27 to 63 mg/l, the content of Cl varies from 104 to 427 mg/l; in the EU18-W3 section: the content of SO ₄ ² varies from 32 to 83 mg/l, the content of Cl varies from 14 to 55 mg/l; and in Nunavut - in the EU18-W4 section: the content of SO ₄ ^{2 -} varies from 8 to 29 mg/l, the content of Cl^- varies from 9 to 20 mg/l; in the EU18-W5 section: the content of SO ₄ ^2- varies from 17 to 44 mg/l, the content of Cl^- varies from 12 up to 33 mg/l.^{[13, p. 103]}

Fig. 10. Ice veins selected on the territory of the Eureka Sound lowland and the Mokka Fjord. (a) Blacktop Outcrop, EU18-W1, (b) Blacktop Outcrop, EU18-W2, (c) Nunavut Outcrop, EU19-W4, (d) Nunavut outcrop, EU19-W5, (e) Mokka Fjord outcrop, MF-W1 to W3. From K.Campbell-Heaton^[13]

The ratio of Cl-/SO ₄ ^2-

In the PLL-5 of the Batagai edoma, the ratio Cl^-/SO ₄ ^2- varies from 0.16 to 1.45, averaging 0.44; in the PLL-7 of the Batagai edoma, the ratio Cl^- /SO ₄ ^2- varies from 0.04 to 1.12, averaging 0.47.

In the PL-17 of the Batagai edoma, the ratio of Cl^-/SO ₄ ^2- varies from 0.18 to 2.31, averaging 0.57; in the PL-20 of the Batagai edoma, the ratio of Cl^-/SO ₄ ^2- varies from 0.45 to 0.93, averaging 0.62.^[10]

Comparing these data with the ratios of chlorides and sulfates calculated by us^[26] in underground ice and surface waters in the north of Western Siberia (Table. 3) note that in terms of the ratio Cl^-/SO ₄ ^2- they are closest to the snowfields in the north of Yamal in the valley of the river.Seyakha (Turbid), where the ratio of Cl^-/SO ₄ ^2- = 0.54, to rainwater in Yamal, where the ratio of Cl^-/SO ₄ ^2- = 1.44, to segregational ice on the first terrace of O.White, where the ratio is Cl^-/SO ₄ ^2- = 1.08. The ratio of Cl^-/SO ₄ ^2- in PLL-5 and PLL-7 sharply contrasts with cryopags (ratio 49.45), most of the Yamal formation ice (68.91; 26.39; 9.77, etc.).

Table 3 . The ratio of chlorides and sulfates in underground ice and possible sources of water supply to them, north of Western Siberia (according to ^[26])

In the veins of the edoma of the Stanchikov Yar, the ratio Cl^-/SO ₄ ^2- varies from 0.57 to 2.90, averaging 1.08.^[11] In the area of Edoma near the village.The Chersky ratio of Cl^-/SO ₄ ^2- varies from 0.52 to 1.11, averaging 0.69. In the water of the Maly Anyui and Kolyma rivers, the ratio of Cl^-/SO ₄ ^2- is 0.01.^[11]

According to the data of K. Campbell-Heaton (Campbell-Heaton, 2020), the ratio of Cl^-/SO ₄ ^2- in the LCL in the Eureka Sound region varies in the EU18-W1 section from 0.19 to 1.30, in the EU18-W2 section from 1.54 to 6.75.

This is not contradicted by the materials given in the work of A.V.Saltykov et al.^[27], devoted to the consideration of the ionic composition of snow cover in Siberia and the Far East, which showed that snow meltwater formed by melting snow cover in hard-to-reach landscapes In North Asia, they are ultra-fresh acidic, slightly acidic and neutral. At the same time, HCO 3– ions prevailed in the ionic composition of the snow cover of Northern _{Asia during the entire observation period}, even near the sea coasts, where SO 4 _{2– and Cl}^– anions intensively enter ^{the atmosphere}. The mineralization of snow cover in many mining regions according to the materials of A.V.Saltykov et al.^[27] is approximately at the same level (from 10 to 35 mg/l). The exception among them is the Ilochno-Su Multinsky and Abakan-Shapshalsky districts, where high values of this indicator were found (61 and 42 mg/l, respectively). The relatively increased mineralization of snow in high-altitude regions is due to the fact that bare areas of bedrock are often found here in winter, contributing to an increase in the left load on the snow cover. It is likely that the formation of the re-vein ices of PZHL-5 and PZHL-7 of the Batagai edoma also occurred at certain moments with a noticeable increase in the introduction of dust to the surface of the snow cover.

Conclusion

1. The mineralization of the Late Pleistocene re-vein ices of PZHL-5 and PZHL-7 of the Batagai edoma varies from 66.56 to 424.8 mg/l, from ultra-fresh to desalinated, the ionic composition of the ice is calcium bicarbonate and corresponds to snow formed under the influence of continental salts.

2. In the dissolved form, Ca ²⁺ dominates among the cations in the studied PPL (PPL-5 from 17.8 to 82.5 mg/l, PPL-7 from 12.0 to 52.1 mg/l), Mg ²⁺ is in second place (PPL-5 from 3.1 to 13.6 mg/l, PPL-7 from 2.6 to 8.3 mg/l).

3. Na⁺ and K⁺ are contained in dissolved form in smaller amounts: Na⁺ – PL-5 from 0.8 to 6.8 mg / l, PL-7 from 0.45 to 4.0 mg / l, and K⁺ – PL-5 from 17.8 to 82.5 mg/l, PL-7 from 1.1 up to 5.6 mg/l.

4. Among the anions, nitrates (NO ₃^{-) prevail}: PLL-5 from 6.9 to 27.9 mg/l, PLL-7 from 5.0 to 54.8 mg/l, the average content of NO3-: PLL-5 14.5 mg/l, PLL-7 12.2 mg/l.

5. PZHL-5 of Batagai edoma, the content of SO ₄ ^2- varies from 2 to 17 mg/l, averaging 6.35 mg/l, the content of Cl^- varies from 1.08 to 7 mg/l, averaging 2.6 mg/l. In the PHL-7 of the Batagai edoma, the content of SO ₄ ^2- varies from 1.4 to 40.5 mg/l, averaging 5.79 mg/l, the content of Cl^- varies from 1.13 to 4.5 mg/l, averaging 1.96 mg/l

6. In the PL-5 of the Batagai edoma, the ratio Cl^-/SO ₄ ^2- varies from 0.16 to 1.45, averaging 0.44; in the PL-7 of the Batagai edoma, the ratio Cl^- /SO ₄ ^2- varies from 0.04 to 1.12, averaging 0.47.

7. The ionic composition of the ice of PZHL-5 and PZHL-7 of the Batagai edoma indicates their formation when filling frost-breaking cracks with water from snow formed under the influence of continental air masses.

8. In some periods, the formation of re-vein ices of PZHL-5 and PZHL-7 of the Batagai edoma occurred with a noticeable increase in the introduction of dust to the surface of the snow cover.

Thanks

The author expresses gratitude to L. V. Dobryneva for performing chromatographic analysis of the ionic composition of the ice, A. Y. Trishin for assistance in conducting field work, as well as L.B. Bludushkina for participating in the design of the work.