Geoforum 17/74 77

Some Peculiarities of Holocene Processes in Western Siberia

Zur Holoziingeschichte der Westsibirischen Torfmoore

Quelques singuliarids des processus holoc&nes sur le territoire de la Siberie occidentale

M. I. NEYSHTADT, L. V. FIRSOV, L. A. ORLOVA and V. A. PANYCHEV, Moscow, Novosibirsk*

Abstract: The authors deal with problems of the origin of peat In the terrttory of the West Siberian Lowland where Holocene processes are sufficiently wtdespread to be representative of this world-wide phenomenon Here, for example, are found the most extensive peat bogs of the Earth The authors deal with the stratlgraphy of these peat bogs and the reconstruction of Holocene conditions in the West Siberian Lowland The development of peat bogs has considerably modified landscape features since the retreat of the last glaclatlon, I.e., during the last 10,000 to 11,000 years The peat bogs began to develop stmultaneously In thousands of depressions after the Ice cover had melted. Later they merged into vast peaty bog regions. Wlthout any mtervention by man the peat bogs will cover all of Western Siberia in the course of several thousands of years The development of extenstve peat bogs IS due to an Irregular advance of floods on Siberian rivers which leads to a rtse In the water level on tributarres of great rivers and to a retardation of the discharge of flood waves In the conclusion the authors point to the problems of economic use of swampy regions and to questions of land reclamation that must be answered before economic use of the terrttory (mainly in connectton with extensive oil and gas deposits m these regions) can be fully effective.

Zunmmenfasrung: Die Autoren befassen such mit der Torfbildung rm Tiefland von Westsiblrlen Hoer smd die gro6ten Torflager der Welt. Aus der Stratlgraphle der Torflager werden die naturlichen Bedmgungen des Holozins in Weststbirlen rekonstrulert. Nach dem Ruckrug def letzten Vergletscherung, d. h. Im Laufe der letzten 10 000 bls 11 000 lahre, hat die Torfbildung den Landschaftscharakter wesenthch umgestaltet. Der VerschlammungsprozeS begann gleichzeltig aus Tausenden von DepressIonen nach Auftauen der Elsdecke. Sle haben such splter zu rieslgen Torfflhchen verbunden inso- fern es LU kemem Emgrtff des Menschen kommt, werden die Torflager In emlgen Tausenden von Jahren ganr Weststbtrien bedecken Der Grund der enormen Vertorfung 1st der unregelmlSige Verlauf des Hochwassers auf den abtrtschen Flussen was iur Stauung des Wasserspiegels an den Nebenflussen gro&r Wasserlaufe und zu emem verlangumten Abfluk der Flut- wellen flihrt Die wlrtschafthche Nutzung des Torfes und die Mehoratton smd eine Voraussetrung zur wlrtschaftlichen Erschlle6ung des Gebietes (msbesondere Im Zusammenhang mlt den rlesigen Erdol- und Erdgasfunden tn dtesen Gebieten)

RCsumC: Les l uteurs traitent les probldmes que soul~ve I’origine de la tourbe sur la tarritoire des Basses Terres de la SibCrte Occident&e OP les processus holoctnes sent suffisamment dtendus pour Ctre reprCsentatifs de ce phbnomane universel. C’est II par exemple que I’on trouve les plus grandes tourbi&es de la Terre. Les auteurs 6tudient la stratigraphle de ces tourbitres, et la reconstruction des conditions Holoc&nes dans les Basses Terra de la SibCrie Occidentale. Le dCveloppement des tourbltres a modifit de faqon consid6rable les traits du paysage depuls le recul de la dernihre glacu- tion, c’est d dire au tours des 10 000 2 11 000 dern&es annCes. Les tourbi&res ont cornmen& a se dCvelopper de faqon simultande dans des mllllers de dCpresslons apr6s la fonte de la calotte glacialre. Plus tard elles ont form6 en se reioignant, de vastes rdgtons P marais tourbeux. Sans I’mtervention de I’homme, les to&i&es devralent recouvrir toute la Sib&be Occidentale dans plusieurs millrers d’ann&s. Le dtveloppement de vastes tourbi&es est dO au dCroulement mdgulier des trues dans les rlv&res slbCrlennes qui conduit d une augmentatton du niveau de I’eau sur les affluents des grands fleuves et i un retard de I’Cvacuatlon des ondes de true. Dons la concluuon, les auteurs se tournent vers le problhne de I’utilisa- tton &onom,que des rigtons mardcageuses, et vers les questtons de r6clamatlon de la terre auxquelles il faut rCpondre

avant que l’utihwtlon lconomique du terrltoire (like principalement dans ces r6gions 3 I’exstence de vastes dCp6ts de p&role et de gaz) puisse devemr vraiment effective.

Holocene sediments cover a wide area on the surface of

the Earth If we take into account only swamp sediments (peat), they cover an area of some l,lOO,OOO km2, of which

715,000 km2 are m the Soviet Union. The correspondmg

* Prof. Dr. M I NEYSHTADT, lnstltute of Geography, Academy of Sciences of the USSR, Staromonetny per. 29, Moscow J-17, Prof. Dr. L V. FIRSOV and others, lnstltute of Geology and Geophystcs, Siberian Branch of the Academy of Sciences of the USSR, Novosibirsk, USSR.

peat reserve amounts to about 240 btlllon tons, of which 157 blllion are m the USSR (NEYSHTADT 1946). As far as sediments of freshwater lakes are concerned (sapropels),

In the USSR alone they cover about 120,000 km2 within the limits of lake water tables, and have an estimated reserve of 259 billion m3, including sapropels in peat

deposits.

In the USSR the largest peat basin is the Lowland of Western Siberia (Fig 1) with an area of approximately

78 Geoforum 17/74

M

m a0

Ntshnevartovsk I

Fig. 1

Locatlon of the extended peat-bog between the lrtish and Ob Rivers, West Siberia

Lagc der ausgedehnten Torfmoore zwischen lrtisch und Ob m Westslbirien

La vastes tourbiCres entre les fleuves lrtlsh et Ob en SlbCrie Orientale

400,000 km2 and peat reserves of 103 billion tons. It IS with justification called a natural phenomenon on a world

scale (NEYsHTADT 1971).

Even the mterfluves of the Ob and lrtysh rivers within the limits of forest and forest-steppe zones seem to be among the most swampy parts of the Lowland of Western Siberia. Marsh plant assoclatlons cover Immense areas in this region.

They alternate with forests and form thus a specific forest-

swamp zone m which marsh formations In some places,

especially In watersheds, dominate over all other types.

During their complicated Holocene development these

marshy phytocenoses coalesced into larger complexes. In this way the largest peat bogs m the world originated,

among which are the peat bogs of Laymenskoye boloto

(502,455 ha), Tsalymo-Yuganskoye boloto (739,200 ha), Katsiyarovskoye boloto (1,321,900 ha) withtn the category

of industrial deposits, and others, Including the world’s

largest peat bog (Bolshoye Vasyuganskoye boloto) covermg nearly the whole mam watershed between the Ob and lrtysh rivers. The total area of this peat bog alone IS

estimated at 53,000 km2.

The well-known Soviet scientist V. I. VERNADSKI (1954) has characterized this marvel of nature in the following way: I’... the Ob and lrtysh with their organic stuff and vegetation remains, with the slow movement of their

quietly flowing waters, with their mouths and deltas, give us a good idea about the begrnnings of carboniferous basm formation.”

It IS interesting to compare the areal extent of the Bolshoye

Vasyuganskoye peat bog with that of some European countries:

Bolshoye Vasyuganskoye boloto peat bog 53,000 km2

Denmark 43,069 km2

Switzerland 41,288 km2

Netherlands 33,780 km2

Belgium 30,514 km2

In the light of our present knowledge the age of this natural

phenomenon is estimated at 10,000 years. Figure 2 pre

sents a cross-section of a peat bog of upland type in Its

Fig. 2

l CornposItion of a peat deposit: 1. upland peat; 2. Sphagnum-Scheuchzeria peat; 3. wood peat (Pinus sibrrka - P. siivstris matl: 4. horsetall . . . and sedge Peat; 5. a thin layer of thoroughly decomposed peat; 6. sandy loam; 7. Humlfied layer; 8. loam; 9. sand; 10. seeds of PMNJS sibirrca; 11 seeds of Menyonthes; 12. stumps and stems in a peaty deposit; 13. Cl4 age; 14. limit of permafrost; 15. admIxture of horsetall; 16. Ap component of Pollen; 17. NAP component of pollen; 18. spores; 19. pollen of water plants; 20. pollen of Pinus silvestris; 21. pollen of pinus sibrrrcu; 22. pollen of spruce; 23. pollen of fir; 24. pollen of larch; 25. pollen of dwarf birches; 26. pollen of birch trees; 27. spores of Sphugrwm; 28. spores of mosses (ffypnaceue); 29. spores of fern species; 30. spores of lycopods; 31. spores of horsetails.

Zusammensetzung einer Torfablagerung: 1. Hochmoortorf; 2. Sphugnum-Scheuchzerw-Torf; 3. Holztorf (Pinus s/b/r/co - P. siivestris); 4. Schllf- rohr-, Schachtelhalm- und Riedgrastorf; 5. ddnne Schicht gut zersetzten Torfes; 6. sandiger Lehm; 7. humlfizierte Schicht; 8. Lehm; 9. Sand; 10. P/flus s/b/r/co-Samen; 11. Meyonthes-Samen; 12. Baumsttimpfe und Aste in emem Torflager; 13. Altersbestimmung mittels Cl4; 14. Grenze des Dauerfrostes; 15. Schachtelhalmbelmtschung; 16. AP-Pollenkomponente; 17. NAP Pollenkomponente; 18. Sporen; 19. Wasserpflanzen- pollen; 20. Pmus siivesrris-Pollen; 21. Pinus sibifku-Pollen; 22. Fichtenpollen; 23. Tannenpollen; 24. Lirchenpollen; 25. Zwergbirkenpollen; 26. Birkenpollen; 27. Sphagnum-Sporen; 28. Hypnuceue-Moossporen; 29. Farnkrautsporen; 30. Bdrlappsporen; 31. Schachtelhalmsporen.

Composition d’un gisement de tourbe: 1. tourbe de fagne; 2. tourbe de Sphugnumbcheuchrerru; 3. tourbe de bois (Pmus s!birica - P. sdvestr/s); 4. tOurbe de roKau, de PrQle et de carex; 5. couche mince de tourbe blen dCcomposCe; 6. glasses sableuses, 7. couche humIf&; 8. plarse; 9. sable; 10. semence de PMWS s/bbhca; 11. semence de Menyunthes; 12. souches et troncs d’arbres dans un gisement de tourbe; 13. ddtermlna- tlon de I’gge exact par C14, 14. limlte du permafrost (perg&ol); 15. addition de prele; 16. APcomposante de pollen; 17. NAPzompounte de Pollen; 18. spores, 19. pollen de plantes aquatlques, 20. pollen de Pinus siivestrls; 21. Pollen de Pinus sibdcu; 22. pollen d’6pccia; 23 Pollen de Pm; 24. Pollen de la% 25. pollen de bouleau nam; 26. pollen de bouleau; 27. spores de Sphagnum; 28. spores de Hypnuceue; 29. spores de foug6re; 30. spores de lycopode, 31. spores de p&le.

M

-1 I-

t\

Geoforum 17174

natural outcrop on the river Ob near the town Nizhne vartovsk in the Tyumen region.

O-O.48 m: Complete upland peat, nearly without decomposition, containing remains of Sphagnum balticurn, Sphagnum dusenii, Sphagnum }ensenii, and from 10 to 20 percent Scbeuchzeria palustris. In the peat are seeds of Pinus sibirica.

0.48 m: Limit of permafrost. All lower deposited peat is permanent- ly frozen (7.8.1970).

0.48-1.20 m: Sphqpnum-Scheuchzeria peat. The quantity of remains of Scheuchzeria ranges from 65 to 90 percent. The Sphagnum genus IS represented by S. angustifoiium, S. jen- sun/i, S. dusenii; pieces of birch and of Pinus bark are com- mon. The peat contams seeds of lenyanthes trifoliata. Degree of decomposition of the peat is about 30 percent.

1.20-l SO m: Pinus sibirica - Pinus siivestrls peat. Remains of both sorts form as much as 85 percent of all peat. P. sibirica in some cases represents as much as 6.5 percent, remams of Sphagnum 5 percent, Scheuchzeria 1 O-l 5 percent, Ericaceae 10 percent, Eriophorum vag/ncltum 5-20 percent. Degree of decomposition of the peat is 40 to 50 percent. In the upper part of this stratum is found the upper woody layer of itumps and stems of trees. The stumps deposited in situ interfere with the above stratum by their upper parts, their roots being in the described woody peat Stems are deposited tightly and form a compact layer The age of one of the stems according to new data is 4050 f 50 years (SOAN- 81 = Sibirskoje Otdelenie Akademii Nauk; C14-Laboratory of the Siberian branch of the Academy of Sciences of the USSR). According to older data this was 3600 f 50 years.

1.50-l .85 m: Sphagnum-Scheuchzerla peat. Degree of decomposi- tion is 20-30 percent.

1.85-3.00 m: Woody peat with remains of birch and comfers. Degree of decomposition IS 40 percent. In the upper part mostly birch Always remains of fquisetum (as much as 50 percent m some cases) and Coax caespitosa. In some places abundant remans of fern species. In this stratum there are two woody layers. The lower layer at a depth of 2.0 m, Is the thicker. It is formed by thick stumps and stems of Betula, Pmus sibirtca, and P. siivestris. A section of stumps and stems has been floated out of the peat. One such stem of the genus Pinus sibwica with its end still in the peat, was abott 57 cm thick in diameter in the hypocotyl and the length of the remaining part of the stem was 240 cm. The absolute age of one stem in this layer IS 6670 f 40 (SOAN- 175).

3.00-3.42 m: Phragmites+Equlsetum-Carex peat, degree of decom- posction about 25 percent. Among reed-grasses C. caespltosa dominates in the upper part (30-80 percent) and C. paradoxa (65-75 percent) in the lower There are also remains of C. strtcta, Caliiergon, Calamagrostis and fern species, only rarely remains of wood plants. Fresh peat IS

red-yellow (orange); exposed to the air it quickly becomes dark and black.

3.42-3.49 m: A thin base layer of peat, black, partly flammable, with Important admixtures of mineral particles.

3 49-4 00 m: Sandy loam

4.00-4 20 m: A humus layer of dark cinnamon color It contains abundant wood remains, mostly birch stems, which can be easily cut by spade. Age for one of the stems, through the application of Cl4 = 10,585 f 80 years (SOAN- 72), or 10,600 *so years (NEYSHTADT, 1971) according to the former measurements.

4.20-4 43 m: Grey-blue loam.

Note: This profile has been published before with only four radiocarbon datinp(NEYSHTADTad SELIKSON, 1971). In the present work, It is published with 13 radiocarbon datings. Some data have been improved.

5oundaries between the individual strata of peat and the mineral substratum are very evident.

The lower part of the peaty deposit presents the structure of valley swamp which becomes valley forest swamp in the central part of the profile and a typical upland peat bog in the upper part.

Up to the present time upland peat bogs of Western Siberia were characterized by an absolute lack of wood stumps and stems in the peaty deposit. We have discovered three layers of thick stumps and stems in this peat bog and in a number of others belonging to the established area according to the geomorphological regionalization. The large stems and stumps are prominent in the peaty deposit (Fig. 3). Of all Western Siberian peat formations the above contains the most information about absolute age.

Fig. 3

Thick wooden stumps in a peat deposit in Western Siberia

Dicke Baumstirmpfe in einem westsibirischen Torfiager

Des troncs d’arbres dans une tourbi&e de la Sib&e Orientate

Geoforum l7/74 81

The profile gives a rather comphcated Image of the develop- ment of vegetation. The lower humified iayer is characteriz- ed by the predominance of birch stems. By its age, - 10,585 f 80 @OAF+1 72), it belongs to Aiiertid, other- wise to Ancjent Holocene. Only in this layer the quanttty of pollen NAP is larger than the AP component.

Consequently the humified layer is replaced by a layer of sandy loam. Later on, throughout two millenma, birch

receded and spruce forests predominated in the preboreal and boreal periods, with an important admixture of larch in the upper part. Ati~ti~um is characterized by the

development of birch forests. As far as the end of this period, varieties of the genus Plnus - Pinus silvestris and P. sibirica -- were not represented cn the composition of

the forests. My former supposition about a late migration of Pinus silvest/ls to the north of Western Siberia

(NEYSHTADT, 1957) has thus been corroborated. in the

subboreal period, Pinus sifvesrr& and Pinus sibiricti spread

very quickly. in this period, Betdaand Pinus sib&c@ had an approximately equat representation, while in subatianti-

cum - in Later Holocene - the absolute predommance

passes to P. sibirka. At the same time, spruce disappears

from the diagram. it is to be noted first that Pmus sib/r/co

populated upland peat bogs and that its seeds are frequent in the upper t/2 m of peat.

It is evident that besides the aut~hthonws elements migrating eiements manifested themselves. The disposi-

tion of pollen of Gramineae, Cyperaceae, and Etrcales in

the peaty deposit corresponds to the changes in its

development.

Together with the stratigraphy of the peaty deposit this diagram presents a number of questions not only in the sphere of climatic changes and the time of origin of the permafrost, but also the growth rate of peat and possible analogies with European peat bogs. if the age of the upper

layer of stems may be correlated with the well-known boundary layer (Grenzhorizont), the age of 3770 years is

really too long for the formation of the upper stratum of

peat of 1 m of depth, just as the age of 545 f 30 years is too long for that of 0.15-0.20 m of thickness. in the latter case attention should be patd to the fact that the upper-

most stratum of peat has been devastated by local construc- tion. if preponderance of Pmus sibmca started at a depth of 0.5 m and has an age of 2850 years, then the same level

of pollen m the diagram of the lower situated peat bog on the watershed of rivers Tshagva and Vasyugan appears 3.5 m deep, corresponding thus to the above mentioned

age and belonging to subatlantlcum, as classified by us some ttme ago.

Mention should be made of the occurrence of seeds of Menyanthes tn Sphagnum-Scheuchzeria peat, as this does not appear in the European part of the USSR and is pro- bably a geographical variant of this sort of peat. The lower

part of the deposit, formed by peat from Phragmites-

Equisetum-Carex, reminds us strongly of the first stages

of swampmg of the surround&g dry land

The data above make evident the grandiose extension of

the Holocene phenomenon in Western Siberia and especiai- ly In Vasyugan. Durtng the last 10 to 11 thousand years

the original landscape was substantially changed after the

retreat of the last glacier.

We must emphasize the extraordinary aggresslvity of this process throughout the entire Holocene. Taking into

account the results of an immense quantity of peat bog research conducted in the European USSR, and also of

materials assembled about the Ob and irtysh river inter-

fluves, we can state that the process of swamping began in the vast areas of Western Siberia more or less simul-

taneously at tens of thousands of independent foci. The

latter depended upon humidity caused by groundwaters in depressions which remained after the retreat of the

glacier and after the decrease of glacial waters. The swamp

foci coalesced and eventually, in a certain period of the

development, merged into a large number of independent and very large peaty massifs. Especially conspicuous was

the process of coalescence of individual peat bogs of Later

Holocene (subatlanticum). This process now goes on automatically without interruption, ~ndition~ by the

accumulation of a large quanttty of water in peat bogs, by the character of peaty vegetation, and by favorable climate, hydrology, and geomorphology.

In some places, however, an interruption of this process is possible due to short and long term climatic deviations

(especially at the end of Middle Holocene - subboreal) or certain georno~~i~i~l conditions.

it is obvious from what has been said up to now, that approximately in a few thousand years, Western Siberia, including the watershed of the Ob and irtysh rivers, will

be totally swamped and covered by peat bogs, except for narrow places on banks of streams, or in higher altitudes,

if the zone nf taiga of the Lowland of Western Siberia is left tn Its present condition.

We have made the first attempts at dlsclosing the speed of the swamping process. With regard to this aim we have

chosen the terltory of the Bakcharskoye boloto peat bog

In the region of Tomsk. Fig. 4 gives a schematic view of the territory between the Bakchar and Shegarka rivers totalling 4,366 km2, out of which 2,268 km2, i.e., 52 per- cent, are covered by swamps ( NEYSHTADT, 1971).

The whole peaty depostt has been divided into five categories: more than 4 m, 4-3 m, 3-2 m, 2-1 m, 1-O m (the zero limit of the peat bog). Taking into account the character of the structure of the upland peat bog we have estimated roughly, for the purpose of an initial orlenta-

Geoforum 17174

Fig. 4

Sketch map of the “Bakcharskoyc boloto” peat-bog near Tomsk

Skrzze der Torfmnore am Bakshar-Flug bei Tomsk

Esquisse de la tourbilre du Bakchar prh de la ville de Tumsk

tion, the age of each category. We have thus arrived at

the foilowmg conclusions (Fig. 4 and Table 1).

The table and the illustration:

1. give an objective example of the gradation of thus

process. It continues actively even at the present time. A certam decrease of the percentage of swamping is due to the fact that the extending peat bog has reached

more permeable land near rivers and terrace steps. The distribution and limits may be seen In the sketch.

Table 1

The age-area relation of Stberian peat

Das Verhaltnrs von Alter und F&he der Sibirischen Moore

La relation Sge-surface des tourbi&es sibdriennes

Peaty deposit m m

Ave. Peat area Peat area Ave. yearly age ha 46 mcrease

34 9000--8000 3200 1.4 32 4-3 8000-6000 33,500 14.7 16.7 3-2 6000-4000 64,000 28.2 32.0 2-l 4000-2000 73,100 32.3 36.5 1-o 2000-O 53,000 23.4 26.5

make clear that this territory (and an overwhelming majority of peat bogs in Western Siberia) originally represented a whole system of independent peat bogs which later coalesced into one vast peaty complex. It

should be noted that this scheme IS drawn on a very generalized scale and that each of its areas is composed of numerous original foci of peat formation.

demonstrate how extraordinarily complex is the develop ment of the peat bog process, which notably depends

upon the character of the relief in the area. As can be

seen in the sketch, the individual tongues of the peat bog seem as if they chose the most suitable parts of the

territory for their advancement, or they stop on the

contrary at the same time in their horizontal expansion, going around higher areas and leaving them as islands

untrl they eventually become covered.

It IS probable that this process has no absolutely unmter-

rupted development. In the individual Holocene periods and in their subdivisions there appeared both explosions of swamp formation and slow-downs of this process. The

uncommon activity of the swamping process is caused In

addition to the above-mentioned reasons, by immense water storage in marshes. The water regime of peat bogs is the result of thousands of years of development under conditrons of a complex interweaving of the vegetation

cover, hydromet~ol~ical factors, and conditions of relief.

Swamps extend in all directions making use of favorable relief. The extent of areas with humidity from ground- water increases year by year as the consequence of in- crease of the total peripheral length of peaty complexes.

The rapid development of peat bogs is linked with the

over~tu~t.~n of Western Siberia. A general hypothesrs

has been pronounced that the substantial oversaturation of this territory is the consequence of a disproportionate

development of flood levels in different zones and regions

of the hydrographical network (basins of Ob and lrtysh

rivers) and of flood backwaters conditioned by them (VENDROV, et id. 1966).

The Holocene peaty sediments of Western Siberia are very

heterogeneous in their typology, in the structure of the peaty deposit, in the quality of the peat, and in their geo- morphological situation. The depth of peat in some cases

attains as much as 10.6 m. Also the vegetatton of peat bogs is varied. It has been described many times (BARANOV, BARYSHNIKOV, BRONZOV, KATS, NEYSHTADT, PYAVTCHENKO, ROMANOVA, and others). Finally, in vast areas a relief built of narrow ridges separated by flat muddy depressions IS developed.

it IS a matter of time that the peat bog with its immense

reserve of peat may play a certain role in developing this territory. Two groups of problems may be distinguished in regard to this particular point:

Geoforum 17174 83

The first group - the use of marshy areas (including peat bogs) for agricultural production, for the formation of meadows, and in forestry. The second group - the use of the storage of peat in varrous branches of industry and agriculture. In a number of cases both groups coincide and we may then speak about the complex use of marshlands.

As an example of the use of peat and marshlands we may mention the Tyumen power plant using peaty fuel, the drainage of 15,000 ha of swamps for afforestation, and the annual extraction of 500,000 tons of peat for the purpose of fertilizing in the Tomsk region.

In any case a proper use of the peat bogs of Western Siberia will be a task of the future, although even present use has been an effective undertaking.

The remodelling of the nature of the Ob-lrtysh interfluve is linked first of all with the drainage and use of marshlands. It can help to solve the problem of po~iati~ this ter- ritory, and give new perspectives to the region for industry, transport, agriculture, forestry, construction of towns, and so on.

NEYSHTADT, M. I. (1946): 7-ortjlonor fondSSSR (Peut Fund of the USSR). Nouchnyy otchct Tsentrainoy torfyonoistontsii za 1941- 1942 gg. Moscow.

NEYSHTADT, M. I. (1957): tstoriyo lesov I pateogeogrofiya SSSR v gotocenye [History of Forests ond Poiocqgeogruphy of the USSR m the Holocene). Moscow.

NEYSHTADT, M. 1. (1968): Resursy saptapeley SSSR i blirhayshiyc zadatshi ikh uutsheniya (The Sappropel Resources of the USSR and the immediate Task of Their Investigation); Tmdy sverdlovr. se/‘.-khoz Inst., 17.

NEYSHTADT, M. 1. (1971): Mimvoy prirodnyy fenoman - zabolotshennost Zapadnn-Sibirskoy ravniny (The World Natural Phenomenon - the Swamping of the West Sierun Plain); lzv. A kod. Nm#k SSSR, seria geogn?f., 1.

NEYSHTADT, M. I. and E. M. SELIKSON (1971): Nate Angaben zur Stratigraphta der Torfmowe Wastsibiriens; Actu agrohu fenmca, 123.

VENDROV, S. L., I. P. GERASIMOV, L. F. KUNITSYN and M. I. NEYSHTADT (1966): Vlagooborot na ravninakh Zapadnoy Siblri yqo rol v formitwanil prirudy i putyi pm- obrazovanya (Water Turn-over on the Territory of Western Siberia and Ways of its Transformatbn); Izv. Akud. Nuuk SSSR, seria geogra/., 5.

VERNADSKI, V. I. (1954): Izbrannyye sotshimniyo (Wetted Works), 1.