STRATIGRAPHY OF PRE-DEVONIAN DEPOSITS IN THE NORTHEASTERN PART OF THE MARIINSK TAIGA (KUZNETSK ALATAU)

B. D. VASIL'EV

(Presented by the scientific seminar of the departments of general geology, historical geology, and combustible minerals)

Comparison of the stratigraphic schemes of the pre-Devonian deposits of the northeastern part of the Mariinsk Taiga proposed by various researchers (Fig. 1) indicates that at the present time

Fig. 2. Stratigraphic column of the pre-Devonian deposits of the region (explanations in the text)

Nikitin D. V.
1927, 1940

Monich V. K.
1937

Anan’ev A.
1940, 1948, 19[[unclear: cropped year]]

\(Cm_{1-3}S_1\)

\(Cm_{2-3}\)

Grauvacke–shale and porphyrite formations

\(Cm_1 + A_2\)

Carbonate sequence

\(S_2?\)

\(Cm_2\)

Turonian sequence

Martaigin Formation

\(Cm_1\)

Limestone sequence with archaeocyaths

\(pCm\)

Shale–limestone formation

Kvarchevo–limestone formation

\(Cm_3 Cm_{1-3}S\)

\(Cm_2 - Cm_3\)

\(Cm_1 + Cm_2\)

\(Cm_1\)

\(Pt_3\)

\(Pt_2\)

Fig. 1. Correlation scheme of the stratigraphic columns of the district

Scale: 250, 500, 1000 m.

Vasil’ev, B. D., 1963

• \(Pt_2\) — Aradanskii limestone
• \(Pt_3\)
• Niiskii horizon
• Ust’-Kundatskii horizon
• Kaidalenovskii horizon
• \(Cm_1\) — Uspenskii limestone
• \(Cm_1 + Cm_2\) — Tyul’ber… limestones with archaeocyaths
• \(Cm_2 = Cm_3\) — Martailenskoe Formation
• \(Cm_3 SS\) — Odarin-Pirozhna Formation

Dembo, T. M., 1948, 1953, 1959

• \(Pt_{2-3}\)
• \(Pt_3^{a}\)
• \(Pt_3^{b}\)
• \(Pt_3^{c}\)
• \(Cm_1 sk\)
• \(Cm_1^2 Blk\)
• \(Cm_2^1 Bzk\)
• \(Cm_2^{2(?)} ml\)
• \(m = 2500–3000\) m

Moskalevskii, A. A., 1958

• \(Cm_1^2\) — Iverinski–Bermament beds, Formation
• \(Cm_2^1\) — Kardzhilasskaia Formation
• \(Cm_2^{1-2}\) — Uspenskii horizon; Tashtagol Formation; Troitsko–Bon-Chachkha Formation
• \(Cm_2^2 - Cm_3^1\) — Martailovo Formation; Upper Tersa Formation
• \(Cm_2^2 Blk\) — Bermament series
• \(Cm_2^1 mk\) — Manakok Formation
• \(Cm_2^2 sch\) — Shaltypinskii Formation
• \(Cm_2^2 Bzk\) — Berikul’ Formation
• \(Cm_3 xt\) — Antonovskaya Formation

Zhuravleva, I. Ts., 1958

• \(Cm_1^1\) — Iramnevestninskie and Tektonicheskie limestones and porphyrites
• \(Cm_1^2\) — Archocyathid limestones:
• massive horizon
• fossiliferous horizon
• Obruchev horizon
• Osykov horizon
• \(Cm_3 + Cm_2\) — Tyugenskii Formation
• \(Cm_2\) — Efundinskii Formation

Apollonov, L. V., 1959

• \(Sn\,en\) — Emseiskii Formation
• \(Cm_1\,\omega S\) — Ustinskaia Formation
• \(Cm_2\,mn_1\) — Munyibashskaya Formation; lower subformation
• \(Cm_2\,mn_2\) — upper subformation; \(m = 300–2000\)
• \(Cm_2 Bl\) — [[unclear: formation name]]
• \(Cm_3 Ol\) — Kitanak Formation

debatable here are not only the questions, common to the Sayano-Altai region, of the lower boundary of the Cambrian and of the nature of this boundary, but also particular questions of the sequence and age of the stratigraphic units distinguished. In the stratigraphic scheme proposed by us (Fig. 2), constructed on the basis of the study of reference sections, medium-scale geological mapping of the area, and detailed mapping of individual key areas, some of these questions find their solution. In general terms this scheme corresponds to the scheme of A. R. Ananyev and is, in essence, a further development of the latter.

Late Precambrian

We assign to the Late Precambrian the strata that lie stratigraphically below the deposits with Cambrian fauna, are separated from them by a break, and are characterized by specific carbonate algal formations. These strata are widely developed within the Kashkadak horst in the central part of the area, and also farther south, where they are exposed in the closure of the anticline by the Kundat and Kiya rivers. The stratigraphic succession of the Precambrian deposits and their composition, with minor changes, are repeated in various sections, which allows us, preliminarily, to subdivide them into four units; with further study these units may possibly be additionally subdivided into formations, or, with clarification of their volume, paleontological characteristics, and mutual relationships, may be raised to the rank of formations.

1. The Kashkadak unit is exposed by the Kashkadak River in its middle course and by the Kiya River below the mouth of the Morozovsky creek only within the limits of the Kashkadak horst. It is gathered into a large, gentle anticlinal fold of northwestern strike, complicated by small folds.

In its lower part, on the Kashkadak River, the unit is represented by black massive fine-grained marbles with a characteristic odor of hydrogen sulfide. Higher in the section they acquire thin bedding, and are then replaced by a member of coarse-crystalline anthraconite marbles with discontinuous thin interbeds of algal dolomites. From this member, from collections by A. R. Ananyev, P. S. Krasnopeeva identified Raduginia contrasta Krasn. and Kabyrsina lamellosa Krasn. Later, from our collections at the same locality, V. A. Shipitsyn identified Conophyton sp. In the upper part of the unit, near the Morozovsky creek, paleontologists of ZSGU found Iussenia sp. in coarse-crystalline black marbles. The incomplete thickness of the Kashkadak unit is estimated approximately at 850 m. The observed boundaries of the unit with younger deposits are tectonic.

1. The Dachny creek unit is exposed by the Kiya River directly near the settlement of Makarak. It is represented by massive light-gray dolomitic marbles, above which lie black fine-crystalline anthraconite marbles containing, at various levels, algal bioherms measuring \(2 \times 5\) meters. The algal rocks of the bioherms are dark-gray marbles with a lenticular-banded texture due to light, discontinuous dolomite interbeds, fractions of a centimeter thick. Stratigraphically above the anthraconite marbles with algal bioherms, at the mouth of Banny creek, lies a horizon of black and dirty-green tuffaceous shales; along its base the lower boundary of the overlying volcanogenic-sedimentary unit is provisionally drawn. The incomplete thickness of the carbonate deposits of Dachny creek exceeds 500 m.

1. The Lower Kundat sequence comprises carbonate and volcanogenic formations with a total thickness of about 800 m, which, on the limbs of the Ust-Kundat anticline and near the settlement of Makarak, lie stratigraphically above the dolomitic and anthraconite marbles of the Dachny Spring sequence. In lithologic composition the sequence may be divided into two parts: a lower, predominantly carbonate part, with three horizons of tuffaceous shales 20–30 m thick in its lower half, and an upper, volcanogenic part. The carbonate rocks of the sequence are represented by dolomitic marbles, graphitic marbles with a fine sprinkling of stellate graphite aggregates, and black “sooty” marbles interbedded with tuffaceous shales. As a rule, they contain nests and veinlets of metasomatically developing quartzite. The marbles directly underlying the volcanogenic rocks of the sequence have been especially strongly replaced.

The volcanogenic rocks of the sequence in the lower part of the noted member are represented by tuffaceous shales, and in the upper part by coarse-clastic tuff breccias, tuffaceous sandstones, and tuffites. Properly effusive rocks within the sequence are rare and are represented by greenstone diabases. On the Kundat River, at the mouth of the Elizavetinka River, the sequence consists of red-colored tuffaceous sandstones and tuffaceous shales with lenses of marble. The effusive rocks of the sequence are represented here by diagenetized orthophyres and albitophyres. On the Kundat River, 1.5 km below the mouth of the Natalyevka River, the volcanogenic sequence is unconformably overlain by conglomerates of the younger carbonate sequence of Deep Spring.

1. The Deep Spring sequence is most fully represented on the limbs of the Ust-Kundat anticline. At the base of the sequence on the Kundat River lies a 20 m-thick bed of conglomerate, which contains large pebbles of black “sooty” marbles, quartzites, and the underlying volcanogenic rocks of the Lower Kundat sequence. Above the conglomerates in the section lie light-gray and dark-gray marbles containing lens-shaped interbeds of black quartzite up to 10 cm thick. Higher up they are replaced by irregularly bedded siliceous-dolomitic rocks, which in certain areas acquire the texture of bedded algal formations of the Collenia type.

A thick, coarse-clastic sedimentary breccia is confined to the middle part of the section of the sequence on the Kundat River; it is composed of fragments of light-gray algal bedded carbonate-siliceous rocks and dolomites cemented by dark-gray carbonate-sandy cement of basal character. The upper part of the sequence is represented by coarsely bedded dolomitic marbles, massive white and bluish dolomites, and yellowish dolomites with thin interbeds of siliceous material.

On the Kundat River below the mouth of the Elizavetinka River, the dolomite sequence, only 300 m thick, lies stratigraphically above the red-colored volcanogenic-sedimentary sequence and has at its base an oncolitic horizon, from which A. G. Pospelov, based on collections by V. V. Elansky, identified Ottonosia aff. columnata (Reitl.), characteristic of the Precambrian of the Siberian Platform.

Lower Paleozoic

The Lower Paleozoic in the eastern part of the Mariinsk taiga is most widely distributed and is represented by the lower and middle divisions of the Cambrian. Deposits of the lower division of the Cambrian, predominantly carbonate, occur only in the southeastern part of the area,

to the southeast of the Kiya fault, whereas volcanogenic-terrigenous formations of the Middle Cambrian division are predominantly distributed to the northwest of the Kiya fault. Within each Cambrian division two formations have been distinguished, namely: the Srednekiya \(Cm_{1}^{1}\ sk\) and Belokamenka \(Cm_{1}^{2}\ blk\), the Berikul \(Cm_{2}^{1}\ brk\), and the Myagkii Log \((?)\ ml\).

1. The Srednekiya Formation, characterized by strong facies variability, lies at the base of the section of the Cambrian deposits of the area. The deposits of the formation are most fully represented on the eastern limb of the Ust-Kundat anticline in the reference section along the Kiya River below Glubokii Creek, where it has a three-member structure with a maximum thickness of up to 800 m and is most fully characterized paleontologically [3]. The deposits of the formation are widely distributed in the basin of the Natal’evka River, but in the facies of carbonate-siliceous shales. Separate parts of the section of the formation are observed along the Kiya River near Myagkii Log, along Glubokii Creek, along the valley of Vas’kin Creek, and in other places. Everywhere the deposits of the formation occur stratigraphically below the massive reefogenic limestones of the Belokamenka Formation. Correlation of sections of the formation from various parts of its distribution (Fig. 3) allows us to draw conclusions about the composition of the formation, its facies variability, and its relationships with other formations. Three types of section of the formation are outlined: the Kiya, Natal’evka, and Kundat types.

The Kiya section of the formation was described by us earlier [3]. Here three large members can be roughly distinguished (from bottom to top).

1. Massive black and light-gray limestones up to 225 m thick, with archaeocyaths of poor preservation in the upper parts of the member.

2. Black platy pelitomorphic limestones with pteropods and brachiopods, with a total thickness of more than 350 m, with a horizon of massive epiphyton limestones up to 65 m thick. From here, on the basis of our collections, H. A. Aksarina identified brachiopods of the genus Philoxenella.

Fig. 3. Scheme of correlation of sections of the Srednekiya Formation (explanations in the text). I — Kundat River, II — B. Natal’evka River, III — Vas’kin Creek, IV — Glubokii Creek, V — Kiya River (reference section), VI — Myagkii Log.

1. Thick-bedded and indistinctly bedded light-gray and dark-gray limestones, replaced in the upper part by platy limestones (20 m) and shales (40 m), with a total thickness of more than 200 m. This member is characterized by archaeocyaths of the “impoverished Bazaikha complex” and by algae.

It should be noted that previous researchers assigned the limestones of the first member to the Precambrian (Yenisei Formation); the platy limestones of the second member were distinguished as the Ust-Kundat Formation by P. A. Ponomarev and others; and the limestones of the upper member with archaeocyaths of the “impoverished Bazaikha complex” were included in the composition of the overlying—

... of the suite of archaeocyathid limestones [7]; at the same time, at the base of the Ust-Kundat Formation (and, accordingly, of the Cambrian) a “conglomerate-breccia” and even a “conglomerate” were described [4], and the upper boundary of the Ust-Kundat Formation with the archaeocyathid limestones was considered conformable. No breaks within the suite of archaeocyathid limestones were noted.

On the basis of geological mapping of a considerable area composed of ancient strata, and of the study of sections in various parts of the region, we came to the conclusion that the Ust-Kundat Formation distinguished by P. A. Ponomarev is only the middle part of a larger natural stratigraphic unit, separated from the underlying and overlying deposits by erosion surfaces and named by us the Sredne-Kiya Formation [3]. The Ust-Kundat Formation is only one of the facies manifestations of the middle part of the Sredne-Kiya Formation (Fig. 3).

In distinguishing the Sredne-Kiya Formation in the above-mentioned scope, we relied on the following facts. In the lower member of limestones (the Yenisei Formation, according to P. A. Ponomarev), on the right side of the valley of the Kiya River, A. E. Kurmeev and we found, along Glubokii Creek, poorly preserved archaeocyathids. Here, along Glubokii Creek, the direct superposition of black platy limestones of the middle member (the Ust-Kundat Formation) upon light-colored massive limestones of the lower member is observed, without any traces of erosion. The “sedimentary conglomerate-breccia” described by P. A. Ponomarev and A. G. Pospelov in the reference Kiya section 1.5 km east of Glubokii Creek, along the strike of the strata, at the base of the Ust-Kundat Formation (and, accordingly, of the Cambrian), is of tectonic origin. The angular character of the fragments of light-gray limestones, the absence of any sorting of the material by size, and the cementation of fragments in the breccia by hydrothermal dolomite, which forms veinlets in the fragments and partly replaces the limestone of the fragments and carries sulfides—all this convincingly testifies to the tectonic nature of the contact between the lower and middle members in the reference section.

The relationship of the limestones of the lower member with the underlying dolomites in the Kiya section cannot be clarified without mining workings, but along the valley of Vaskin Klyuch, 2.5 km west of the settlement of Makarak, at the base of the lower member of light-gray limestones, red-colored limestone conglomerates more than 30 m thick have been exposed, testifying to erosion before the deposition of the Sredne-Kiya Formation.

The middle and upper members of the Sredne-Kiya Formation in the reference section occur conformably, but when traced along the strike into the area of Bolshaya Natalyevka they are facies-replaced by carbonate-siliceous shales. The upper member in the reference section is unconformably overlain by archaeocyathid limestones of the overlying Belokamenka Formation, the lower horizons of which everywhere have an uneven pink coloration due to the reworking of an ancient weathering crust. The paleontological characterization of the Sredne-Kiya Formation according to data from the reference Kiya section was given by us earlier [3].

The Natalyevka section of the formation is characterized by a reduction in the total thickness of the formation to 550 m, with a reduction in the thickness of the lower member of limestones to 120 m (Fig. 3). The section of the second type is composed predominantly of carbonate-siliceous shales (“layer cake”), and in its upper part of volcanogenic rocks, and is characterized by manganiferousness, especially in areas where volcanogenic rocks are developed. Paleontologically, the second type of section has so far been characterized very poorly: it is characterized by skeletal elements of sponges (siliceous interbeds) and by the mass development of the algae Proaulopora and Botominella (carbonate interbeds).

The Kundat section of the formation differs in that here, with...

at the mouth of the Sobolinka River, on Precambrian dolomites, lies a unit of gray and black marbles, sandy and dolomitic, with a total thickness of 300 m. In the upper third of the unit a 20 m horizon of dirty-green tuffites is distinguished, interbedded with marbles. At the base of the unit and immediately beneath the tuffite horizon there are two beds of stromatolitic marbles. From the lower bed, P. S. Krasnopeeva identified Collenia kundatensis Krasn. from collections by A. R. Anan'ev. From this same unit, A. G. Pospelov identified Renalcis sp., Osagia sp. from collections by V. V. Ellanskii.

Thus, the Middle-Kiya Formation in the section along the Kiya River, with a thickness of up to 800 m, is represented essentially by platy limestones with brachiopods, above and below which occur packets of archaeocyathid limestones. In the Bol'shaya Natal'evka area the formation has a thickness of up to 550 m and is represented by carbonate-siliceous shales. In the section along the Kundat it has a thickness of only 300 m and is represented by stromatolitic dolomitic marbles. The Lower Cambrian age of the formation is determined by its fauna [3].

2. Belokamenka Formation. Under the name Belokamenka we describe a formation of massive, predominantly light-gray archaeocyathid limestones, lying stratigraphically above the Middle-Kiya Formation; that is, in its scope it differs sharply from the previously described Belokamenka Formation [5] and Belokamenka Series [9], which included all carbonate deposits of the area, including Precambrian ones (Fig. 1).

The most complete section of the formation is exposed by the Kiya River for a distance of 6 km, directly in the area where the Bol'shaya and Malaya Belokamenka and Berikulya streams flow into it. The lithologic composition of the formation is very uniform: it is characterized by light-gray or white limestones with archaeocyathid fauna and algae. However, the formation also contains black bituminous limestones devoid of fauna; these occur sporadically in the lower part of the formation section, where they separate small reef-like swells of light-colored limestones with fauna (Bol'shaya Natal'evka). The lower horizons of the formation are characterized by limestones “with pink streaks,” that is, unevenly colored in pink tones by an admixture of red-colored pelitic material, indicating erosion of an ancient weathering crust and the transgressive occurrence of the Belokamenka Formation. The thickness of the formation is provisionally estimated at 2500 m. The formation is characterized by archaeocyathids, trilobites, algae, and spores. The archaeocyathid assemblage is defined as pre-Sanashtryk-Gol’gian; however, elements of the Sanashtryk-Gol’gian fauna appear in the section of the formation from its very base [3].

3. Berikul' Formation, as described by us, in its scope corresponds to the Martaitinskaya Formation of V. K. Monich [11], the porphyrite unit of T. M. Dembo [5], the Berikul' Formation of A. A. Mossakovskii [9], and the upper subformation of the Mundybash Formation of L. V. Alabin.

Volcanogenic rocks of the Berikul' Formation are widespread in the east of the area, where they participate in the structure of the large Berikul' syncline of submeridional trend. The formation lies with sharp angular unconformity on the underlying carbonate units of the Lower Cambrian and Precambrian and is distinguished by more gentle fold forms. At the base of the formation lie horizons of lava breccias with a mass of fragments of the underlying rocks. Higher in the section of the lower part of the formation appear horizons of tuffaceous rocks of basic composition, interbedded with greenstone diabases and diabase porphyrites. Above the latter lie coarse-grained labrador porphyrites and their tuffs, form—

… formed in separate areas (the headwaters of the Belokamenka River) under subaerial conditions. Higher in the section of the suite, diabase porphyrites predominate, with rare horizons of pyroclastic formations. In the basin of the Bogotuyul River, in the west of the area, the upper horizons of the suite are represented by albitophyres and their tuffs; here the thickness of the suite reaches 3000 m. The Berikul suite is overlain by the substantially terrigenous Myagkii Log suite, the lower horizons of which are well expressed in the area of Veselaya Gorka on the watershed of the Kiya and Dudet rivers.

1. The Myagkii Log Suite, in its volume, corresponds to the tuff-sandstone suite of T. M. Dembo [5], the Shaltyr suite of A. A. Mossakovsky [9], the lower subsuite of the Mundybash suite of L. V. Alabin, and the sedimentary-pyrogenic sequence of A. R. Ananiev.

The deposits of the suite are widely distributed only in the northwestern part of the area, beyond the Kiya fault, where they compose the limbs of the large Tuluyul anticline and the Myagkii Log syncline associated with the latter. In the Veselaya Gorka area they rest with erosion on the underlying porphyrites of the Berikul suite and are represented, according to V. K. Monich, by graywacke conglomeratic sandstones and clayey shales. The suite is composed mainly of greenish-gray graywackes, sandstones, and shales, among which there are horizons of tuffites, porphyrites, and, very rarely, lenses of marbles. In the core of the Myagkii Log syncline, thin-bedded green-violet shales and siltstones predominate. Judging from their composition, the rocks of the suite are products of erosion of the underlying volcanogenic formations of the Berikul suite. Paleontologically the suite has not been characterized. Its thickness reaches 1250 m.

Questions of Age and Correlation

Of the pre-Devonian sequences described above, only three have a paleontologically substantiated age. Thus, the most ancient, the Kashkadak sequence, is of Precambrian age, since it contains Conophyton sp., which, according to I. K. Korolyuk [10], occurs only in Precambrian deposits. The Srednekia and Belokamenka suites are characterized by archaeocyathan fauna, the Cambrian age of which is beyond doubt. However, most of the stratigraphic subdivisions described contain no paleontological remains that would make it possible to date these deposits reliably, and therefore their age can for the present be determined only by comparison with suites of other areas analogous in composition and stratigraphic position (Fig. 4).

The age adopted on this basis is indicated in the stratigraphic column (Fig. 2).

REFERENCES

1. L. V. Alabin. On the structural-facies zones of the Lower Cambrian in the northwest and north of the Kuznetsk Alatau. Geologiya i geofizika, No. 4, 1963.

2. A. R. Ananiev. On the question of the Cambrian and Precambrian in the Mariinsk taiga of the Kuznetsk Alatau. Transactions of the Mining-Geological Institute, West Siberian Branch, Academy of Sciences of the USSR, issue 2, 1948.

3. B. D. Vasiliev, V. D. Kamelina. On the Kiya reference section of the Lower Cambrian. Materials on Mineralogy, Petrography, and Mineral Resources of Western Siberia, issue 3, Tomsk University Press, 1965.

4. M. K. Vinikman, A. B. Gintsinger. On the question of the correlation of Cambrian deposits of the western part of the Altai-Sayan folded region. Materials on the Regional Geology of Siberia. Transactions of SNIIGGiMS, issue 24, 1963.

5. T. M. Dembo. Stratigraphy of the Lower Paleozoic of the northern part of the Kuznetsk Alatau. Bulletin of the Moscow Society of Naturalists, Geological Section, vol. 34, issue 5, 1959.

6. G. M. Ekhanin. On the stratigraphy of Sinian-Cambrian formations of the Sarala River area. Materials on the Geology and Mineral Resources of Krasnoyarsk Krai, issue 2, Krasnoyarsk Geological Administration Press, 1961.

Fig. 4. Correlation scheme

Visible labels in the correlation chart (left to right):

• Yenisei Series

• Mountain Shoria and Kuznetsk Alatau
  after Popov et al., 1960, 1962

• Bolshekitat Series
• Mundybash Series
• Ulutag Series
• Mazas Series
• Mrass Series
• Karchit Series

• Ust-Anzas Series

• Mountain Shoria, Kamzas
  [[unclear: “Sivoz”]] et al., 1964

• Ulutag Series
• Kurlan Series
• Sakharov Series
• Adiak Series

• Pyankovo Series

• Kuznetsk Alatau
  R. K. Vasil’ev, 1964

• Maikogo Loga
• Berikul Series
• Belokamensk Series
• Srednekies Series
• Kaz-Kyzym (?)
• Dolomites of Kl. Glubokii
• Nizhnekundat Series
• Kl. Dachnyi

• Kashkadak Series

• Kuznetsk Alatau
  R. S. Yekhanin, 1961

• Taimdon Series
• Syya Series
• Usin Series
• Kondom Series
• Belyi Series
• Upper part
• Gidrin dolomites
• Dolomites

• Beds with Newlandia

• Kuznetsk Alatau
  R. B. Ivankin et al., 1964

• Koshkulak Series
• Malokoshkulak Series
• Bezymyannaya Series
• Efremkino Series
• Kolodzhul Series
• Tardzhul Series
• Kulburtstog Series
• Poludennaya Series

• Kaoteg Series?

• Batenyov Ridge
  Tomashpolskaya, 1964

• Verkhneerba Series
• Sladkie Koreni
• Yulin Series
• Chenokov Series
• Bagrad Series
• Sonskaya (?)
• Loshchenkov Series
• Kudeteikh Series

• Goldzha Series

• Kh. Azyrtal

• Tolcheinsk Series
• Azyrtal Series
• Solontsov Series
• Kuten-Bulun Series
• Upper part \(C_2\text{–}O_5\)
• Martyukhin Series
• ?
• Bidzha Series

1. I. T. Zhuravleva, L. N. Repina, V. V. Khomentovskii. New data on the stratigraphy of the Lower Cambrian of the Mariinsk taiga. Dokl. AN SSSR, vol. 123, No. 6, 1958.

2. G. A. Ivankin, I. I. Koptev, V. E. Nomokonov. On the stratigraphy of the region of the Kulbyurstyug River (eastern slope of the Kuznetsk Alatau). Geology and Geophysics, No. 4, 1964.

3. Ya. G. Kats, B. N. Krasilnikov, A. A. Mossakovskii, E. D. Sulidi-Kondratiev, N. N. Kheraskov. Stratigraphy of the Paleozoic deposits of the Minusinsk Basin and its mountain framing. Tr. VAGT, issue 4, 1958.

4. I. K. Korolyuk. The significance of stromatolites for the stratigraphy of the Cambrian and Precambrian, as exemplified by the south of the Siberian Platform. Tr. Interdepartmental Conference on the Development of Unified Stratigraphic Schemes of Siberia. 1956.

5. V. K. Monich. Geological sketch of the Berikul gold-mining district. Tr. Trust “Zolotorazvedka” and the NIGRIZoloto Institute, issue 7, 1937.

6. D. V. Nikitin. Stratigraphy and tectonics of the Mariinsk taiga of Tomsk Governorate. Zapiski Ross. Miner. ob-va, part 56, issue 1–2, 1927.

7. D. V. Nikitin. Geological structure and mineral resources of the northwestern part of the Kuznetsk Alatau. Tr. TsNIGRI, issue 124, 1940.

8. A. G. Pospelov, N. A. Aksarina, A. S. Boyarinov, Yu. S. Nadler, E. S. Fedyanina. On the stratigraphy of the Cambrian of Mountain Shoria. Materials on the Geology and Mineral Resources of Krasnoyarsk Krai, issue 1, Publishing House of the Krasnoyarsk Geological Administration, 1961.