Bog Waters of Tomsk Oblast

N. M. Rasskazov, P. A. Udodov, A. D. Nazarov, T. Ya. Emel’yanova

Bog (peat) waters are widely distributed within the territory of the West Siberian Lowland and exert a substantial influence on the formation of river and subsurface (groundwater) runoff and of the microclimate of the region, on the conditions for developing oil-and-gas-bearing, iron-ore, and bauxite-bearing districts, and on the development of agriculture, forestry, peat extraction, and other branches of industry. Peat waters and peats possess valuable balneological properties and can be used, along with other mineral groundwaters, for therapeutic purposes. In addition, peats can be widely used as organic and microfertilizers (especially lowland peats), and as fuel, bedding, and litter material.

The main volume of fieldwork on the subject considered in this article was carried out by the authors jointly with geological and design-and-exploration organizations in Tomsk and Novosibirsk (northern part) oblasts. In connection with this, the data proposed for discussion pertain mainly to the indicated regions.

Hydrogeochemical investigations of peat deposits, conducted systematically by the authors since 1963, are comprehensive in nature and include the study of the dynamic equilibrium system water—gas—underlying rock—peat as a whole [5, 6, 7, 8].

Sampling of water, gas, rocks, and peat for various types of analysis was carried out in accordance with generally accepted methods [3, 9] during route surveys at characteristic peat deposits. In order to reveal the interrelation between bog waters and deeper groundwaters, and changes in the composition of waters and peats with depth, shallow boreholes and pits were widely used.

The geology and hydrogeology of the regions characterized; the lithological composition of the deposits underlying the peat; and the areal distribution of the different types of peat deposits and accumulations have been described with extensive use of archival materials from the Novosibirsk and Tomsk Territorial Geological Administrations and the institute “Giprotorfrazvedka,” with which the authors collaborated on a contract basis.

1. General information on the region’s bogged territories

The bog massifs of the region characterized, according to data from the institute “Giprotorfrazvedka,” are represented mainly by raised and lowland peat deposits, with subordinate

in the distribution of transitional and mixed types. At the same time, a certain zonality is observed in the development of different types of peat deposits, consisting in the replacement, from south to north, of lowland and transitional peatlands by raised bogs. The exceptions are modern and ancient river valleys, where lowland peatlands are predominantly developed.

It should be noted that almost all transitional and raised peat deposits contain, at their base, a layer of lowland peat. Interbedding of different types of peat is often observed. In the composition of the deposits underlying the peat on watershed areas, in the indicated direction there is likewise a regular replacement of clayey rocks with elevated carbonate content (up to 13% CaCO$_3$) by sandy-clayey rocks with carbonate content up to 0.5% (Table 1). In this case, the areas of development of lowland peatlands coincide with the area of distribution of underlying rocks of elevated carbonate content.

The composition of the peat of lowland deposits, as determined by G. G. Yasnopolskaya, a staff member of Tomsk State University, is mainly sedge–hypnum, sedge–woody, sedge, and mire–forest; that of transitional deposits is sedge–sphagnum; and that of raised deposits is sphagnum.

The ash content of peats increases toward the lowland types; moreover, lowland peats of floodplain deposits have a higher ash content (up to 50%) than lowland peats of watershed deposits (26.5%). This probably also explains the higher content of microcomponents in the peats of lowland deposits (Table 2). The input of microcomponents into peats occurs for the most part together with clay particles of eroded rocks, which are more enriched in microcomponents (Table 1).

When peat deposits are fed by mineralized groundwaters, the latter will also exert a considerable influence on the enrichment of peats with microcomponents (Table 3). In addition, part of the microcomponents is introduced together with atmospheric precipitation (Table 3). In turn, the selective capacity of plants and physicochemical conditions lead to the redistribution of microcomponents among peats, waters, and clay particles.

II. Composition of the Waters of the Region’s Waterlogged Territories

The formation of the composition of the waters and peats of peat deposits is conditioned by the influence of geological, physicogeographical, geomorphological, hydrogeological, hydrogeochemical, and other factors that determine the rate of peat growth, the feeding of bogs, the mineralization of peat waters, and other conditions.

In the region under consideration, it is important to take into account the geomorphological conditions of occurrence of peat deposits. In this connection, the authors propose distinguishing valley, watershed, and ancient-valley peat deposits.

In turn, among the valley deposits one should distinguish floodplain and terrace (of low and high terraces) deposits, with the latter subdivided, according to the composition of the underlying rocks, peats, waters, and gases, into smaller taxonomic units. Approximately the same can be said with respect to peat deposits of watersheds and ancient valleys (Table 4).

Since atmospheric, surface (river and flood) and groundwaters participate to varying degrees in the feeding of peat deposits, below, alongside the peat waters, a characterization of these waters is also given.

Table 1

Average content of microcomponents and carbonates in Quaternary rocks of the region

Content of microcomponents in bog deposits (in % of air-dry mass) of region 2

Table 2

Table 3

Content of microcomponents in waters of the waterlogged territory of the region

Mean values, mg/l

Continuation of Table 3

Table 4

Classification scheme of peat deposits of the region

Macrocomponent composition of waters

The macrocomponent composition was studied according to the generally accepted method [9]. The results of the analyses are summarized in Table 5. In characterizing the composition of waters, the authors used the Aleksandrov–Shukarev classification. Atmospheric (snow and rain) waters have an acidic medium, a mixed ionic composition, and low mineralization (up to 15 mg/l).

River waters are characterized by a mixed ionic composition, a slightly acidic to slightly alkaline medium, mineralization of 58–296 mg/l, and free CO₂ content from 2.2 to 22 mg/l. Iron was not observed. Ammonium was recorded up to 2 mg/l. The amount of suspended particles in the Ob River in spring reaches 2–3 g/l.

Table 5

Overall chemical composition of bog waters of the territory of the region

Flood snow waters in spring are characterized by an acidic medium, a mixed ionic composition, and mineralization of 100–170 mg/l. The amount of suspended particles reaches 10 g/l. Flood rain waters in summer are characterized by a neutral medium, a mixed ionic composition, and mineralization up to 253 mg/l. The amount of suspended particles was recorded on June 31, 1968, in the area of the village of Trubachevo as equal to 12.3 g/l.

Groundwaters participating in the feeding of floodplain and terrace peat deposits have a neutral medium, a hydrocarbonate-calcium composition, and mineralization reaching 436.7 mg/l. The iron content reaches 2.1 mg/l, ammonia—2 mg/l, and free CO₂—29 mg/l.

The waters of different peat deposits are distinctive in composition. The waters of floodplain lowland peat deposits, which have flood and groundwater feeding, are distinguished by the greatest mineralization (250–410 mg/l). This can also explain the increased iron content in the waters (up to 2.0 mg/l). The content of ammonia and free CO₂ in the water reaches, respectively, 0.56 and 48.4 mg/l. The medium ranges from slightly acidic to slightly alkaline. The water composition is hydrocarbonate-magnesium-calcium.

The waters of lowland terrace peat deposits, characterized by groundwater and partly atmospheric feeding, have mineralization up to 212 mg/l. The medium is slightly acidic. The composition of the waters is most often hydrocarbonate-calcium. Transitional terrace deposits, having impeded groundwater feeding, are characterized by a slightly acidic medium (pH 5–6), mineralization up to 50 mg/l, ammonia content up to 6 mg/l, free CO₂ up to 30 mg/l, and iron (at individual points) up to 0.2–0.3 mg/l.

Raised terrace deposits have mainly atmospheric feeding, an acidic medium (pH up to 4.0), low mineralization of 18–36.4 mg/l, and a mixed ionic composition. The ammonia content was recorded up to 10 mg/l, free CO₂ up to 37 mg/l. Iron in the waters is noted at individual points in an amount of 0.2–0.3 mg/l.

For the waters of watershed lowland peat deposits, a slightly acidic medium, a low content of free CO₂ (20 mg/l), ammonia and iron, a hydrocarbonate-magnesium-calcium composition, and mineralization of about 76 mg/l are characteristic. The waters of transitional watershed peat deposits have a mixed ionic composition, an acidic medium (pH 5.0), and low mineralization (up to 33 mg/l). Iron was not detected. The waters of watershed raised deposits are characterized by a mixed ionic composition, low mineralization (18–20 mg/l), an increased content of ammonia (up to 10 mg/l) and free CO₂ (up to 55 mg/l); iron is not noted.

It is thus evident that peat waters differ substantially from other ground and surface waters in macrocomponent composition. At the same time, different types of peat deposits are characterized by a specific composition of waters [5, 7].

Microcomponent composition of the waters of the region’s waterlogged territories

The microcomponent composition of the waters was studied according to the methodology of the Tomsk Polytechnic Institute [14]. From the analysis of Tables 1–4 it is evident that peat waters may be enriched with microcomponents both at the expense of waters (atmospheric, surface, and ground) and at the expense of leaching of rocks and decomposition of the peats themselves. The data obtained are summarized in Table 3. From the table it is evident that peat waters are characterized by a wide—

with a complex of microcomponents; a certain specificity is also revealed in the distribution of microcomponents in the waters of peat deposits of different types.

Gas Composition of Bog Waters

The composition of free and dissolved gases in peat waters was studied with a VTI-2 instrument and an KhL-4 gas chromatograph [3]. Free gas was sampled by the generally accepted method, and dissolved gas with the aid of Savchenko’s bottle [3].

The groundwaters feeding floodplain lowland peat bogs have a carbon dioxide–nitrogen composition of dissolved gases. In the waters of peat deposits the methane content sharply increases, and in terms of gas composition the water type becomes nitrogen–methane. An elevated methane content is noted in the waters of raised deposits (71–90%) as compared with lowland deposits (37–67%) (for free gases of the upper 20–25 cm of the active peat layer). At greater depths the composition of dissolved gases (from squeezings) is substantially methane-rich.

Composition of Dissolved Organic Matter in Bog Waters

Study of the organic substances of peat waters by the method of I. V. Tyurin [13] and with the aid of an electron microscope [1] shows that, first, the total content of organic matter ($C_{\text{org.}}$) in peat waters is higher than in groundwaters; second, in the waters of raised deposits $C_{\text{org.}}$ is higher (up to 107 mg/l) than in the waters of lowland deposits (up to 25 mg/l); and, third, organic matter exerts a great influence on the migration of microcomponents in peat waters, forming with the latter various organic compounds (humates, fulvates, and others).

Isotopic Composition of Hydrogen in Bog Waters

It is difficult to judge the distribution of deuterium in the waters of peat deposits of the region under consideration, both because of the small number of samples studied and because of the influence of atmospheric precipitation, whose isotopic composition is subject to considerable fluctuations.

In general, atmospheric precipitation is depleted in deuterium as compared with groundwaters. Snow waters are especially depleted in deuterium. At the same time, a sharp increase in the deuterium content in rain waters has been recorded after a prolonged break in precipitation. In this case, the first “portions” of rain are most enriched in deuterium.

Peat waters for isotopic composition were sampled simultaneously on August 23, 1968, at two neighboring deposits (a lowland and a raised one) in the area of the village of Srednii Vasyugan, from a depth of 20 cm. During the period preceding sampling, precipitation in the form of drizzling rain had occurred repeatedly. During the last twenty-four hours there had been no rain. Analysis of the waters by the densimetric method showed an increased deuterium content (+1.3) in the water of the raised peat deposit and a decreased content (−1.6) in the water of the lowland peat deposit relative to the standard (water of the Tom River). An increased deuterium content (+1.2) was also noted in the water of the Aleksandrovskoe raised deposit, examined on July 16, 1968, during a prolonged break in precipitation. However, it is still premature to draw any conclusions on this question.

Microbiological Composition of Bog Waters

The microflora of peat waters and peats was studied by the nutrient-media method [10] at the Maloe Taganskoe deposit by engineer V. A. Shamolin of the Problem Geological Laboratory of the Tomsk Polytechnic Institute. He notes a high activity of bacteria—8.7 thousand ammonifying bacteria, 4.1 and 2.2 thousand bacteria assimilating mineral nitrogen, and fungi—in the upper (to 10 cm) peat layer, and a decrease in activity with depth, as well as fluctuations in activity depending on the season. The regime microbiological observations that were carried out showed that whereas in March the total number of ammonifying bacteria in one part of moist peat at depths of 10 and 20 cm was respectively 72 and 1.2 and 0.4 thousand, and bacteria decomposing cellulose were not observed at all, in June ammonifying bacteria were recorded in an amount of 987 thousand at a depth of 10 cm and 81.9 thousand at a depth of 20 cm; bacteria assimilating mineral nitrogen, respectively, 1400 and 196 thousand; bacteria decomposing cellulose—170.4 and 13.1 thousand; and fungi—11.8 and 5.8 thousand.

In the raised watershed Novo-Vasyugan deposit, the main mass of microorganisms belongs to microscopic fungi. Spore-forming bacteria were found in insignificant quantity; deeper than 50 cm the water and peat are almost sterile.

III. Composition of Pore Solutions of Peats and Underlying Rocks

The pore solutions of peats and underlying rocks were studied by the method of P. A. Kryukov [2] only at the Aleksandrovskoe and Sredne-Vasyuganskoe deposits. The Aleksandrovskoe deposit is composed, from the surface down to 55–80 cm, of raised-bog peat, and below (to 100 cm) of lowland peat. On July 16, 1968, peat samples were taken at depths of 20, 55, and 100 cm and loams at a distance of 30 cm from the peat bottom.

Study of the composition of the pore solutions of the peats showed that with depth the mineralization increases from 20 to 121.4 mg/l (the latter was noted in lowland peat), while \(C_{\text{total}}\) decreases from 320 to 24.3 mg/l. It was also noted that \(C_{\text{total}}\) decreases with an increase in the load during squeezing of the pore solutions (from 305.1 mg/l at 5 kg/cm² to 105 mg/l at 30 kg/cm²). The deuterium content in the pore solution of sample No. 2 (load up to 20 kg/cm²) is lowered (−1.3) relative to the standard. The composition of the dissolved gas, released by vacuum extraction with the aid of a special device from the pore solution squeezed from a special peat sample taken from depths greater than 55 cm, is methane and, more rarely, nitrogen–methane.

The pore solution of the underlying rocks has a higher mineralization of 334.3 mg/l and a very low value of \(C_{\text{total}}\) (2.2 mg/l). The Sredne-Vasyuganskoe deposit is situated on the sands of the floodplain terrace of the Vasyugan River and is composed mainly of raised-bog peat. During examination of this deposit on August 24, 1968, with the aid of pits and shallow boreholes, it was recorded that the groundwater level lay 90–120 cm below the peat bottom. The sands beneath the peat, to depths of 20–85 cm, were colored brown. Below the colored layer, and outside the deposit and from the surface, light-gray sands, ferruginized in places, occur. The pore solutions of the colored sands contain 36.4 mg/l of organic matter (\(C_{\text{total}}\)); the light-gray sands, 3.6 mg/l; and the peat, 237.3 mg/l.

At present it is still difficult to draw any conclusions regarding the pore solutions. Only certain features of their composition have been outlined. These investigations are continuing.

Composition of Aqueous Extracts from Underlying Peats of Rocks of Elevated Carbonate Content

Distilled and peat water (Aleksandrovskoe raised-bog deposit) were used as the initial solvent, in the amount of 900 ml per 300 grams of dry heavy loam with a carbonate content of 13% (as CaCO₃), taken from the Vasyugan massif at a depth of 7.0 m. An increase is observed in the mineralization of the waters to 220 and 434 mg/l, free CO₂ to 14 and 29 mg/l, and NH₄ to 0.2–0.6 mg/l, which indicates the possibility of an increase in the mineralization of meteoric waters when they come into contact with rocks of elevated carbonate content. In addition, the composition of the aqueous extracts indicates the possibility of enrichment of peat waters with microcomponents of the rocks.

IV. Questions of the Methodology of Hydrogeological and Hydrogeochemical Investigations of the Region’s Waterlogged Territories

The indicated hydrogeological and hydrogeochemical features enabled the authors to develop a new methodology for hydrogeological investigations of the waterlogged territories of the region under consideration, with the aim of draining them [8]. In contrast to the previously proposed methodologies [4, 12, 11], it is recommended here that the number of hydrogeological boreholes in the area of development of clayey underlying rocks be significantly reduced, both at the stage of preliminary and at the stage of detailed investigations. Boreholes here should be drilled only to refine the boundaries of the various districts.

At the same time, in the northern districts, despite the predominant development of raised-bog peat deposits, one should expect the submersion of the deposit by weakly mineralized groundwater of the underlying sediments, and therefore a reduction in the number of hydrogeological boreholes is inadmissible. The authors also noted that places where deeper groundwater discharges into bogs are recorded by the anomalous composition of peat waters. Thus, for example, examination of such a discharge near the village of Kislovki shows the following:

a) peat waters removed from groundwater discharge points and only weakly affected by the latter do not contain divalent iron. Their mineralization is 373.3 mg/l; the bicarbonate-ion content is 283.6 mg/l; trivalent iron, 0.3 mg/l; ammonium, 2.3 mg/l; manganese, 45.3 μg/l; strontium, 27.2 μg/l;

b) peat waters under the influence of ascending groundwater have a mineralization of 382.1 mg/l; divalent iron content, 3.0 mg/l; trivalent iron, 1.6 mg/l; bicarbonate ion, 383 mg/l; manganese, 136.4 μg/l; strontium, 43.1 μg/l.

This indicates the possibility of using the composition of peat waters in searches for discharge sites of deeper groundwater and, consequently, for substantiating the location of hydrogeological boreholes. Presumably, areas of discharge of deep groundwater can be identified during the interpretation of aerial photographs by chains of lakes, the emergence of rivers and streams from bogs, or by darker areas of the photographs, usually associated with more humid sites [7].

In addition, the hydrogeochemical investigations carried out in the Kolyvan-Tomsk folded region showed the possibility of using the composition of peat waters and peats to identify areas of ore mineralization and to trace fault disturbances. When deep groundwater emerges at the day surface, the latter loses, as a result of changes in physicochemical conditions, some of its components in the form of carbonate, oxide, sulfide, arsenate, and other compou—

also as a result of sorption and other processes. A considerable role here is also played by the biological geochemical barrier, since usually the places of discharge of deep horizons are waterlogged. Bog deposits in these places have a high ash content (up to 83%). Together with calcium carbonates there precipitate mercury, cadmium, silver, lead, iron, copper, and barium, the solubility products of whose carbonates are lower than that of calcium, as well as nickel, zinc, manganese, antimony, and arsenic. The latter are probably sorbed. Together with iron hydroxides there precipitate manganese, titanium, phosphorus, barium, arsenic, chromium, cobalt, lead, strontium, zinc, and nickel. Thus, for example, in the area of the villages of Yashkino—Litvinovo, on the basis of elevated contents in the waters (including bog waters), exceeding the background by a factor of 10, of lead, copper, zinc, and mercury, a zone of sulfide mineralization has been outlined [15].

An attempt was also made to study the hydrocarbon and isotopic compositions of bog gases for the purpose of prospecting for oil and gas deposits (gas surveying). Gas analysis of samples of bog gases taken along a profile at the Sovetskoe oil field showed the absence in them, within the sensitivity limits of the instrument used (KhL-4), of noticeable amounts of heavy hydrocarbons. Data on the isotopic composition of the carbon of bog gases have not yet been obtained.

V. Questions of drainage of the region’s waterlogged territories

The hydrogeological and hydrogeochemical investigations carried out make it possible to regionalize the waterlogged territories of the region described according to drainage conditions. Peat deposits of modern river valleys, which have complex recharge conditions with a predominance of groundwater recharge, have been assigned to the most difficult to drain. When they are drained, it is necessary to intercept groundwater and floodwaters and to lower the head of the waters of the underlying aquifer. The periodic inundation by river waters in high-water years must also be taken into account.

Also classified as difficult to drain are watershed peat deposits underlain by sandy and sandy-clayey deposits, and peat deposits of ancient valleys. These deposits have groundwater and atmospheric (rain and snow) recharge.

Watershed peat deposits underlain by a thick stratum of clays, but having a great peat thickness (up to 10.0 m), have been assigned to the type of medium drainage difficulty.

Watershed peat deposits underlain by a thick stratum of clayey rocks, but having a peat thickness of up to 4.5 m, have been assigned to the comparatively easily drained category.

VI. Questions of the use of peat waters and peats in the national economy

The authors do not dwell on the generally known facts of the use of waters and peats for medicinal purposes, of peat as a handicraft, bedding, and fuel material, and as an organic fertilizer.

Additional investigations carried out by the authors have shown the possibility of using peat as a microfertilizer and as a starting product for obtaining the preparation “torfot” [7].

Thus, for example, at the Maly Tagansky deposit the peats contain microcomponents assimilable by plants in quantities sufficient for application to the soil.

The preparation “torfot,” isolated from peat by the method of the Odessa Institute of Eye Diseases named after Filatov by an engineer of the Tomsk Poly-

of the Technical Institute by V. A. Shamolin, underwent clinical testing at the Tomsk Medical Institute. The greatest effectiveness (69–71%) was noted for “torfota” from lowland peats, and the least (45–50%) for raised-bog peats.

Conclusions

Thus, the hydrogeological and hydrogeochemical studies carried out on the bogged territories of the region under consideration make it possible to view a number of questions in a new way.

The waters of peat deposits are groundwater and, depending on specific conditions, may be assigned either to perched water or to ground water.

Floodplain lowland peat deposits (the Ob and others) usually have a constant hydraulic connection with the underlying groundwater and may be regarded as the upper part of the first aquifer (the groundwater horizon).

The waters of terrace (Bolshoe Taganskoe and others) and watershed (Sredne-Vasyugan and others) peat deposits, occurring on soils with good filtration properties, have either a permanent or periodic hydraulic connection, or are perched. Therefore, the assignment of the waters of a given deposit to ground water or to perched water must be decided concretely in each case. Watershed peat deposits occurring on clayey soils (the Vasyugan peat massif and others) are isolated from other aquifers by a thick stratum of clays and therefore constitute the first aquifer (the groundwater horizon).

Certain features of the formation of peat deposits are also emerging [7]. If the predominant influence of mineralized groundwater on the formation of lowland floodplain and terrace peat deposits is beyond doubt, the same cannot be said of the formation of lowland watershed peat deposits. In general, in the development of peat deposits in the region described, one may distinguish lowland, transitional, and raised-bog stages. This is also indicated by the presence of a layer of lowland peat at the base of raised-bog and transitional deposits. This can also explain the present-day diversity of types of peat deposits in the region. From this point of view, the presence of lowland peat deposits on the Vasyugan massif may be explained by a prolonged lowland stage of development, caused in turn by the increased carbonate content of the underlying rocks (up to 13–20% CaCO₃). As a result of the leaching of salts from rocks and peats by waters of atmospheric origin, the mineralization of the latter increases. The possibility of an increase in the mineralization of waters at the expense of salts from rocks is also confirmed by the experiments carried out.

LITERATURE

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