Tertiary Deposits of the Tomsk Area

B. V. Plotnikov

(Presented by the Department of General Geology)

One of the first researchers to draw attention to the deposits of sands lying on the clay shales of the Lagerny Garden outcrop was I. D. Chersky [9]. He assigned these sands to the Jurassic age. In 1894 A. N. Derzhavin indicated that the sands of Lagerny Garden, lying on clay shales of Carboniferous age, are Tertiary. In 1910 A. M. Zaitsev noted that the Tertiary deposits in the system of the Tom River occupy an extensive area. These deposits are exposed along the Tom River near Tomsk and east of the Tom River along the Basandaika, Ushaika, and B. Kirgizka rivers.

The sands assigned to the Tertiary age, with interbeds of sandy clay, contain impressions of leaves of dicotyledonous plants and lie beneath post-Pliocene yellow sand with pebbles. Comparing the sediments encountered on the Tom River below Lagerny Garden with Miocene-age sediments on the Chulym River and near the village of Simonovo, A. M. Zaitsev considers them to be of the same age [4].

According to A. M. Zaitsev, the Tertiary deposits of the area under study are sediments of an extensive freshwater basin.

The Tertiary deposits of the Tomsk area have been studied in greater detail by M. E. Yanishevsky [21], E. V. Shumilova [20], K. V. Radugin [12, 13], V. A. Khakhlov [17, 18], L. A. Ragozin [14], R. S. Ilyin [5], P. A. Nikitin [11], B. V. Mizerov [8], and M. G. Gorbunov [1].

V. A. Khakhlov [18], describing the fossil Tertiary flora of the Tomsk area, came to the conclusion that the Rezhenka beds and the Tomsk fossil flora of Lagerny Garden include a large number of identical forms of flora, which he dates as Upper Eocene or, possibly, Lower Oligocene.

The presence in the Eocene deposits of a certain number of subtropical plant forms, now found in eastern China and Japan, allowed V. A. Khakhlov to conclude that the Eocene had a moderately mild climate.

In 1930 V. A. Khakhlov noted the heterogeneity of the Tertiary deposits of the Tomsk district and indicated that their lower horizons may prove to be Upper Cretaceous.

K. V. Radugin [12, 13], dealing mainly with the genesis of the Tertiary deposits of the Tomsk area, indicates that the Tertiary deposits near the village of Rezhenka, lying almost at the level of the Bolshaya Kirgizka River, are hypsometrically situated several tens of meters lower than those horizons.

which were studied by M. E. Yanishevsky beneath the Camp Garden. As regards the genesis of the Tertiary deposits, K. V. Radugin denies their lacustrine or lacustrine-fluvial origin and regards these sediments as deposits of “the channel, floodplain, and oxbow lakes of a large river analogous to the Tom’ River.” This is indicated by “the oblique bedding of the clays” and “well-washed channel sands, the inconstancy of lenses of allochthonous lignite contaminated with sand and silt, and other features.”

According to K. V. Radugin [13], “the fluvial and lacustrine Tertiary deposits were formed from redeposited products of Mesozoic and Tertiary weathering, almost everywhere veneering the Paleozoic rocks.”

R. S. Il’in [5], studying the Tertiary sands and clays of the Camp Garden, considered them to be of fluvial origin, and identified the flora he found as close to the modern flora of the Mediterranean Sea (with a mean annual temperature of \(+10^\circ\)).

E. V. Shumilova [20], on the basis of mineralogical analysis of the loose sequence of the classic section of the Camp Garden in the Tomsk area, precisely established the boundary between the Tertiary and post-Tertiary sediments, dividing the sequence into the following 5 horizons.

I. Terraced post-Tertiary sequence from horizon “A” through horizon “K,” inclusive.

II. Tertiary sandy-clayey bedded sediments, in the lower horizons with plant remains.

III. Redeposited kaolinized rocks, dirty-white and white clays with quartz fragments, with weak bedding.

IV. Eluvium of clay shales.

V. Carboniferous clay shales.

The section of the Tertiary sequence is represented by the following lithological varieties of rocks:

1) horizon “L”—cross-bedded sands passing into clays of brownish-gray color;

2) horizon “M”—sands and clays with plant remains;

3) horizon “N”—interbeds of sand with peat;

4) horizon “O”—sandy gray clay. The thickness of the entire sequence fluctuates within 8–9 m.

B. V. Mizerov [8] and others distinguish two stratigraphic horizons among the Camp Garden Tertiary deposits:

a) lower—clayey; b) upper—sandy.

a) Lower horizon

The lower horizon of the Camp Garden deposits lies on the weathering crust of clay shales of Carboniferous age.

This horizon is composed of grayish-bluish clays that include thin interbeds of fine-grained sand.

In the lower parts of the same horizon, lenses of dense yellowish-brown sand contain remains of flora.

The flora of this horizon was first studied in detail by M. E. Yanishevsky [21], who identified the following forms: Taxodium distichum miocenum Hr. Pinus sp. Myrica (Comptonia) driandroides Und. Populus bolsamoides goepp., Juglans acuminata abr., Juglans densinervis Schm., Carpinus grandis Und, Corylus cf. insignis Hr., Fagus cf. antipofii Hr., Gulreus cf. nimrodi Und. Gulreus groenlandica Hr., Liquidambar europalum Abr., Nyssa sp. Diospyros bachysepala Abr.

On the basis of the determinations cited above, M. E. Yanishevsky assigned these deposits to the Miocene age. A. A. Larishchev, studying brown coals (lignitized plant stems) lying on the hori-

in the zone of grayish-blue clays, assigns an Oligocene age to the brown coals of the Lagernosadskoye deposit.

A. A. Nikitin [11], on the basis of the phytodetritus and seed flora collected from lenticular interbeds, establishes that these deposits are of Oligocene age.

V. N. Sukachev [15] determined pollen of the following plants from this same horizon: Pinus typ. silvestris, Pinus ex. Seet. strobus, Salix, Alnus, Betula, Pterocarya, Ulmus, Quercus, Tilia, Ilex.

The pollen determined by him is pollen of an Oligocene-age flora.

b) Upper horizon

The upper stratigraphic horizon of the Lagerny Sad Tertiary deposits is composed of light quartz sands, in which gentle oblique bedding of river type is clearly visible.

In the upper part of this horizon the sands are finer-grained and silty, with a yellowish tint. The yellowish coloration of the sand is due to thin films of iron oxides.

At the top of the horizon there occur small lenses of white clay and thin interbeds of plant remains.

This horizon is well traced eastward and northeastward in boreholes of the manometer and instrument plants.

P. A. Nikitin [11], studying the seed flora of this Upper Oligocene horizon, determined in it the following species composition: Azolla ventricosa sp. nov., Salvinia sp. exot (cf. S. rubereulata P. A. N.), Picea sp. exat., Pinus ex. subgen. Haploxylon, Sequoia Couttsiae Heer, Taxodium parvispermum sp. nov., Typha sp. (exat), Sparganium sp., Potamogeton pygmaeus Cnandl. Potamogeton cartiocosus sp. nov., Potamogeton sp. 3 (exot), Potamogeton sp. 4 (exot), Alisma sp. 1., Alisma sp. 2., Carex sp. 2, Carex sp. 3, Scirpus sp. 1, Scirpus 2 (exot), etc.

V. A. Nikolaev [10], on the basis of the stratigraphic correlations presented by him, also confirms the Oligocene age of the Lagerny Sad Tertiary deposits.

Mineralogically, both stratigraphic horizons were well studied by E. V. Shumilova [20] and B. V. Mizerov [8].

We shall cite only certain data concerning the mineralogical composition of the upper and lower stratigraphic horizons of the Paleogene of Lagerny Sad (after B. V. Mizerov).

B. V. Mizerov [8], carrying out a mineralogical analysis of the two horizons, points to their similarity in composition (Table 1).

Dividing them into fractions, he notes that among the light fraction the predominant mineral is quartz, which accounts on average for 66%. The quartz grains are weakly rounded; the angular parts of the grains have even edges. Feldspar accounts on average for 23%. The feldspar grains are more rounded than the quartz grains. The percentage content of feldspar grains in the light fraction with grain size less than 0.25 mm increases and, conversely, that of quartz decreases.

Micas make up on average 4–7% and are represented by biotite and muscovite. Muscovite occurs as well-rounded plates, biotite as small flakes of irregular shape, sometimes rather strongly decomposed. In the fraction with grain diameter greater than 0.25 mm the mica content reaches 9–10%.

Among the light fraction, chlorite, kaolinite, and other minerals are present.

Among the heavy minerals, in the fraction with grain diameter less than 0.25 mm, ore minerals predominate; their amount is on average about 45%, among

Table 1

Percentage content of minerals of the heavy and light fractions of Paleogene deposits (after B. V. Mikerov)

among which magnetite and limonite occur most often, more rarely pyrite and ilmenite. The ore minerals are weakly rounded.

Of the epidote group, epidote and zoisite occur most often; together they account on average for 34%.

Among the other minerals of the heavy fraction there occur: green hornblende—9%, garnet—3%, zircon—4%, tourmaline—2%, apatite, sphene, rutile, disthene, anatase, brookite, siderite.

Comparing the mineralogical characteristics obtained for these horizons of Lagernyi Garden with the deposits of more ancient horizons of Tertiary age, B. V. Mizerov came to the conclusion that the Tertiary deposits of Lagernyi Garden cannot be older than the Oligocene, and that these sediments correspond to the time of the retreat of the Paleogene sea and the establishment of a continental regime under the conditions of the West Siberian Plain.

New data on the age of the Tertiary deposits in the area of the city of Tomsk are given by M. G. Gorbunov [1]. Studying the Tertiary deposits of the Rezhenka depression, M. G. Gorbunov notes that the Tertiary deposits near the village of Rezhenka, which had previously been dated to a single age—the Eocene—can at present be divided into 3 suites differing in age. The oldest is the Kasparan suite, consisting of loose sands with seams of brown coal up to 5.0 m thick and interbeds of gray and white clay. In the roof of the distinguished suite M. G. Gorbunov found seeds and fruits of the following plants: Pinus Thomasiana (göpp), E. Reichenbach, Pinus palaeostrobus (Ett.) Heer, Pinus Petri sp. nov., Sequoia sp., Taxodium sp., juglans, Kryshtofovichii gorb., Corylus sp., Magnolia cor Lucbvig, and others.

On the basis of the listed forms of fossil plants, M. G. Gorbunov considers that the age of the deposits of the Kasparan suite may be dated as the lower part of the Middle Oligocene.

On the eroded surface of the Kasparan suite lies the younger Rezhenka suite, described by V. A. Khakhlov and dated by him as Upper Eocene. Therefore M. G. Gorbunov shifts the age of the Rezhenka suite to the upper part of the Middle Oligocene.

The third suite of Tertiary deposits is exposed at the Kasparan Yar; it is composed of sand with thin interbeds of gray and yellow clay, which also lies on the eroded surface of the deposits of the Kasparan and Rezhenka suites. M. G. Gorbunov, correlating this suite hypsometrically with the Tertiary sediments of Lagernyi Garden, is inclined to assign it to the Upper Oligocene.

Up to the present time, the Tertiary deposits concealed beneath the sediments of the first terrace of the Tom River in the area of the settlement of Cheremoshniki and beneath the sediments of the seventh terrace, distributed in the area of the Khromov quarry, the “Sibir” match factory, and in the area of the “Baktin” experimental farm, remain completely unstudied.

Boreholes drilled in the area of the settlement of Cheremoshniki (Fig. 1, V), the yeast plant (Fig. 1, B), and the psychiatric hospital (Fig. 1, A) reveal beneath the Quaternary deposits a loose sandy-clayey sequence about 50 m thick. Hypsometrically, the roof of these sediments in the area of the settlement of Cheremoshniki lies more than 40 m lower than the Tertiary deposits of Lagernyi Garden. The sequence of Tertiary age penetrated by boreholes in the Cheremoshniki area can stratigraphically be divided into 3 suites, sharply differing in their lithological-mineralogical composition.

The upper suite (Fig. 1, A, B, V) is represented predominantly by clayey varieties of rocks. In its roof the suite is composed of gray clays with rare and thin interbeds of fine-grained sand. The basal part of the suite is composed of fine-grained kaolinized sand, including lenses of vari-grained, gravelly ...

Borehole 1257

Depth, m: 0.0; 10.0; 20.0; 30.0; 40.0; 50.0; 60.0; 70.0; 80.0; 90.0; 100.0; 110.0; 115.5

A

Borehole “Bronzovaya”

B

Borehole 1255

C

Outcrop of the Khromovo quarry

D

Conventional symbols

• clay
• loam
• sandy loam
• clayey shale and sandstone
• sand
• sand with pebbles
• weathering crust
• gravel and sandstone

Fig. 1.

sand, white clay, and lignite. The thickness of this formation beneath the first terrace ranges from 15–20 m and increases to 45–50 m beneath the high terraces. Within the limits of the first terrace this formation lies beneath the lower parts of the Kasparan Formation of M. G. Gorbunov [1]. We distinguish this formation as an independent Tsymlian Formation, with a presumed Lower Oligocene age.

The upper boundary of this formation in the Tomsk area is traced rather clearly in a number of boreholes (the yeast plant, the chemical-pharmaceutical plant, the state mill, etc.), where the boundary passes between the basal pebble beds of the first terrace of the Tom’ River and the loams of the Tertiary deposits. We distinguish the lower boundary of the Tsymlian Formation on the basis of facies and lithological-mineralogical features.

The granulometric composition in the top of the formation is predominantly pelitic (57–58%), while in the bottom it is sandy-aleuritic (90–99%).

The mineralogical composition of the heavy fraction in the top and bottom of the formation differs somewhat. The content of ore minerals ranges from 16% in the top to 46% in the bottom, leucoxene from 11.5 to 25% in the sandy bed, and zircon from 6 to 14%. However, the content of some minerals of the heavy fraction increases in the opposite direction, i.e., from the bottom of the formation toward its top. Thus, for example, the epidote content ranges from 2 to 45%, hornblende from 0 to 11.5%, etc.

Among the minerals of the light fraction, quartz and feldspar are most widespread, and in the top of the formation the content of these minerals is somewhat higher than in the bottom.

The second formation is predominantly sandy, where a bed of medium-grained sand includes lenses of quartzites and quartzitic sandstones that, macroscopically, differ little from the quartzites of Tugan. Evidently, this formation may be called the Tugan Formation, with a presumed Eocene age.

The upper part of the formation consists of greasy gray clay with small lenses of lignite, which downward pass into silty gray loams with small lenses of fine-grained sand. The thickness of this bed is not maintained and ranges from 0 to 10 m.

The lower part of the second formation consists of sandy varieties of rocks (from fine- to medium-grained in composition). The content of the sandy fraction (0.5–0.25 mm) ranges from 76.26 to 88.0%.

The mineralogical composition of the heavy and light fractions of this formation differs from the formation described above by an increased content of ore minerals, ranging from 42% in the top of the formation to 58% in the bottom. Here a relatively increased content of pyrite and siderite is observed. The ore minerals are characterized by weak rounding. In the clayey varieties of rocks of the formation, an increased content of leucoxene (20%) is observed and, conversely, a decreased content of zircon (4%), epidote-zoisite (1.4%), and hornblende (1.4%). Apatite, tourmaline, and disthene occur in very small amounts. In the light fraction, quartz predominates over feldspar.

In thin interbeds of silty clays confined to the sands of this formation, a spruce-cone scale was found. According to the determination of M. G. Gorbunov, this scale may be assigned to the Middle Paleogene. Thus, the Eocene age of the Tugan Formation is confirmed.

The Tugan Formation, which includes quartzitic sandstones, correlates well with the Lyulinvor Formation of the stratigraphic scheme of the Tertiary deposits of the southern part of the West Siberian Lowland.

According to the description of I. G. Zal’tsman, this formation is widely distributed in the northern and central regions of the lowland, in the area of the Chuya Depression in the Altai, and is also noted in the Baraba and Kulunda—

...in the Dinskaya steppes, is represented by opokas and quartzitic sandstones. This member may serve as a marker for compiling local stratigraphic schemes and sections dated as Eocene.

The third member of the loose Tertiary sequence, lying at the base and penetrated by boreholes in this area, is composed of kaolinized quartz gravelly sand, the thickness of which ranges up to 10 m. The fraction with particle size 0.25–0.5 mm accounts for 58.26%; 0.5 mm—19.84%; 1.0–2.0 mm—13.25%; and more than 2.0 mm—7.39%. The remainder falls in the fraction less than 0.25 mm.

The mineralogical composition of this member, like its granulometric composition, differs sharply from that of the overlying Tuganskaya Member. Here there is a reduced content of ore minerals, fluctuating within 38%, very little pyrite, and siderite is completely absent. An increased content of leucoxene (23%) and zircon (20%) may be noted. Among other minerals of the heavy fraction there occur epidote-zoisite—2.5%, hornblende—2.5%, pyroxene—3%, apatite—2.5%, mica—1.5%.

Among the light fraction the predominant mineral is quartz, which accounts for 40%. The feldspar content is 21%. The quartz and feldspar grains differ from the quartz and feldspar of the overlying members by their weak rounding and angular form of the fragments.

On the basis of the foregoing, we distinguish this member as an independent Cheremoshinskaya Member. Its age, in all probability, will be Paleocene or Upper Cretaceous, as V. A. Khakhlov [17] assumed.

The Tertiary deposits exposed by the Khromovka quarry and ravine (Tomsk-II area) occupy a higher hypsometric position than the Tertiary sediments of the settlement of Cheremoshniki (Fig. 1, Г). The elevation of the Tertiary sediments of the Khromovka quarry above the Tertiary deposits of the area of the settlement of Cheremoshniki is about 80 m, and above the top of the Lagernosadsky Tertiary deposits—25–30 m. The total thickness of the Tertiary deposits of the Khromovka quarry is no less than 40.0 m. The lower part of the section is typical Lagernosadskaya. It is composed of fine-grained kaolinized sand with thin lenses of light-gray loam, described in detail above.

On the eroded surface of the Lagernosadsky deposits lie sandy beds. At the base they are composed of coarse-grained gravelly, poorly rounded sand and gravel, in places cemented by oxides of iron and manganese. The thickness of this member ranges within 6.0–6.5 m.

At the base of the member a lens of greasy brown clay was encountered, with imprints of flora resembling leaves of maple, horsetails, and other plants. This member is called by us the Khromovskaya Member.

The mineralogical composition of the upper—Khromovskaya—and lower—Lagernaya—members differs from one another. The content of ore minerals in the concentrate in the Khromovskaya Member ranges within 40–50%, leucoxene—17–20%, zircon—1.7%, epidote-zoisite—5–20%; an increased content of garnets is observed, reaching 23%, brown mica—4.2%.

In the Lagernaya Member of the Khromovka quarry there is a somewhat reduced content of ore minerals—35–40%, leucoxene—5–10%, garnet—2.5–5%, but an increased content of zircon—8.9% and minerals of the epidote-zoisite group—26–35%.

In their composition, structure, and facies characteristics, the Tertiary deposits differ sharply from the overlying Quaternary deposits.

In the area of the city of Tomsk, the upper boundary of the Tertiary deposits is distinguished rather clearly, since all Quaternary sediments within the city of Tomsk and its environs are represented by terraces of the Tom River and its tributaries, at the base of which, as a rule, basal pebble beds occur.

The lower boundary of the Tertiary deposits should be considered the weathering crust of Paleozoic clay shales and sandstones, since the Cretaceous deposits on the right bank of the Tom River in the Tomsk area are distinguished only conditionally.

Thus, the areas of distribution of Tertiary deposits within the city, in comparison with previous data, have expanded considerably and can be contoured in the southern part of the city by the boundaries of the sixth and seventh terraces; in the northern part—in the area of Cheremoshniki and the psychiatric hospital—the Tertiary deposits form the basement of the first, third, fourth, fifth, sixth, and seventh terraces.

Beneath the third, fourth, and fifth terraces of the right bank in the southern part of the city, the Tertiary deposits were evidently washed away by erosional cycles; during the formation of the terrace deposits, a thick Quaternary sequence lay on the eroded surface of Paleozoic clay shales and sandstones. Proceeding from the above, it seems to us that for the Tomsk area one may adopt the stratigraphic scheme of the Tertiary deposits given in Table 2.

Well-expressed cross-bedding, lenticular occurrence, a thick sequence of washed quartz sands, and also the presence of dark-brown clays with inclusions of lignite lenses make it possible to assign the Tertiary deposits to the lacustrine-river type.

M. K. Korovin [6] wrote that “the Tomsk Tertiary basin was a freshwater lake, the shoreline of which passed near the city of Tomsk. Probably, at that time conditions of a very warm climate prevailed in the Tomsk district.”

According to A. N. Krishtofovich [7], at the beginning of the Tertiary period the flora of the Tomsk area was of a moderately warm climate.

According to L. A. Ragozin [14], within the Tomsk area the Paleogene was an epoch of accumulation of continental sequences, and throughout this entire epoch full-flowing rivers ran in the Tomsk area and there were many quiet, swampy lakes, along whose shores luxuriant broad-leaved woody vegetation grew, characteristic of a warm, humid climate close to the climate of the modern Caucasus.

Studying the features of the formation of the Tertiary deposits of the Tomsk Ob region, B. V. Mizerov [9] notes two main stages of sedimentation—the Eocene–Oligocene and the Miocene–Pliocene.

In the Eocene and the first half of the Oligocene epoch, sedimentation took place under weak-flow and stagnant lacustrine-bog conditions, while in the second half of the Oligocene the lacustrine-bog environment was replaced by a lacustrine-river one, under which the upper horizons of the Lagernosad Oligocene deposits were formed.

In the Miocene–Pliocene epochs the right-bank zone of the Tom River changed from an area of sediment accumulation into an area of removal of Tertiary material.

The great diversity in the composition of the sediments, their sharp boundaries, visible dips of the strata, etc., indicate that the accumulation of Tertiary sediments is connected with oscillatory movements of the Earth’s crust in the Tomsk area.

L. A. Ragozin associates with the movements that appeared in the Neogene the formation of one of the important regional tectonic structures

Table 2

Stratigraphic scheme of the Tertiary deposits of the Tomsk district

area—the so-called Tomsk swell, which has a latitudinal extent.

According to the conclusions of M. A. Usov [16], in Western Siberia, at the Paleogene–Neogene boundary, the Savian phase of tectogenesis manifested itself, dissecting the relief that had been smoothed in the Paleogene.

In stratigraphic schemes compiled by various authors for the Mesozoic and Tertiary deposits of the West Siberian Lowland, it is noted that the Neogene lies on the eroded surface chiefly of the Lower Oligocene. This once again confirms the correctness of M. A. Usov’s conclusions regarding the manifestation of the Savian phase of tectogenesis at the Neogene–Paleogene boundary.

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