ON THE QUESTION OF THE AZYRTAL, SUYARYK, AND OTHER FAUNAL COMPLEXES

V. D. TOMASHPOLSKAYA

(Presented by the scientific seminar of the departments of general geology, historical geology, and mineral resources)

On the Batenev Ridge and the Azyrtal Range, deposits with the Azyrtal and Suyaryk faunal complexes are combined by us into the Yulinian (Azyrtal) suite.

As is known from the author’s works [2, 6, 7, 8], in the area of the Sukhiye Solontsy hollow the Azyrtal suite rests with a conglomerate at its base upon the carbonate Usinsk suite, in which, near the top, there is the Obruchev trilobite complex, first established by us in 1957 [2]. In the section across the summit of the mountain with elevation 803.5 at point 1054, etc. [6], and also in the section across the eastern part of the same mountain at point 1554, in beds occurring at the top of the Usinsk suite, in 1957–1960, with the participation of R. T. Bognibova and students of the GRF during educational geological field practice, a rich trilobite fauna was collected. The identifications made by us at that time were known to the broad geological community from reports at conferences of TPI and from photographic plates distributed to geological organizations, and were partially published. A complete list of the fauna from these sections was given by R. T. Bognibova without references to us [1, p. 92], although the identifications were made only by us.

In the stratotype of the Obruchev horizon, established as early as 1925–1927 by Ya. S. Edelstein, A. G. Vologdin, and E. V. Lermontova on Mt. Dolgii Mys, a large number of faunal localities are now known, in which a large and, in terms of genera and species, diverse complex of archaeocyaths and trilobites is established; for this complex we retain the name “Obruchev.” As can be seen from the lists of trilobites given in Table 1, it includes the same forms that are characteristic of the upper parts of the Usinsk suite at Sukhiye Solontsy.

Within the overlying Azyrtal suite we distinguish two subsuites: the lower, with the Azyrtal faunal complex, and the upper, with the Suyaryk complex.

In the stratotype at Sukhiye Solontsy we assign to the lower subsuite of the Azyrtal suite a sequence consisting, from bottom to top, of conglomerates, sandstones, siliceous and clayey shales, lenses and packets of limestones. The conglomerates occurring at the base consist of subrounded and rounded pebbles and boulders of effusive rocks of intermediate and basic composition, as well as blocks and pebbles of organogenic limestones of the underlying sequence. The thickness of the conglomerate packet is very heterogeneous: in the section across the summit of the mountain with elev. 803.5 it is 70–80 m; eastward

their thickness sharply decreases to several meters, while westward it increases noticeably to several hundred meters, and then they make up almost the entire lower subformation (Mt. Odinochnaya), while limestones and beds of terrigenous rocks form irregular lens-shaped bodies within them.

In the section through the summit of the mountain with elevation 803.5, where the thickness of the conglomerates is 30–50 m, above them lie thin-bedded siliceous shales, argillites, and sandstones with lenses of limestones and beds of calcareous conglomerates. On the northern slope of the eastern summit of the mountain with elevation 803.5, in the limestones that occur over the extent of the terrigenous-carbonate bed and have a thickness of 140–160 m, remains of trilobites were collected at several points (pts. 1548–1543) (Table 1), which we take as the stratotype of the Azyrtal complex. To this it should be added that in the Azyrtal complex we also include remains of trilobites collected from lens-shaped bodies of massive limestones occurring among conglomerates or among terrigenous rocks (pts. 606, 609). The composition of the trilobites in them, as is evident from Table 1, is characterized by the presence of almost all forms typical of the Obruchev horizon of the upper Usun Formation, while the general list of trilobites of the Azyrtal complex (as is evident from Table 2) in the stratotype contains: forms known in the Obruchev and in the so-called “Solontsy horizon” (according to L. N. Repina), and isolated genera of the Amginian Stage: Chondranomocare, Proasaphiscus, Gaphuraspis, Amgaspis, Kootenia, with an obvious predominance of Solontsy forms.

To the upper subformation of the Azyrtal Formation we assign deposits of almost the same lithological composition, which are exposed in the hinge part of the syncline, while trilobite remains were collected in a bed of massive gray limestones in the southern part of the mountain with elevation 726.1 (pts. 1501, 1503, 22, 23). This complex was named by us the Suyaryk complex and is characterized by a noticeable predominance of Middle Cambrian genera. As is evident from Table 2, by the beginning of Suyaryk time the numerous genera and species that appeared in the Obruchev horizon and even earlier and passed in the same composition into the Azyrtal horizon disappear entirely, such as: Bonnia globosa Tomaschp., Eocorynexochus convexus Tomaschp., Edelsteinaspis ornata Lerm., Batenoides Repina, Solontzela Rep., Onchocephalina Rep., Olenophalus conspectus Tom.^1, Onchocephalites salebrosus Tomaschp., Eosipeneia, Repina, several species of the genus Kooteniella. Such Middle Cambrian genera as Olenoides optimus Laz., Kootenia vologdini Lerm., Chondranomocare bidjensis Polet., Granularia obrutchevi Polet., Erbia sibirica (Schm.), Kooteniella slatkowskia (Schm.) acquire a dominant role. By the beginning of Suyaryk time the archaeocyaths also disappear. In the works of geologists of SNIIGGiMS [3] this complex is called the Karasuk complex.

On the Batenyov Ridge, analogues of the Azyrtal Formation are represented by a substantially carbonate sequence and are exposed in several sections. On the NW limb of the Katyushka syncline, on the deposits of the carbonate Usun Formation, on beds with the Sanashtygol faunal complex, according to the data of the Son party [4, 5], limestones of the Bogoyul Formation^2 lie with a break and unconformity; in them, near the base in light massive limestones and higher up in dark platy limestones, trilobites were identified which, in our opinion, have every basis for being called the Azyrtal complex, as is evident from Table 2 by the presence of such forms as Edelsteinaspis ornata, Proerbia, Onchocephalina, Laminurus, Chondranomorace, and others. Apparently, the Katyushka effusives of the mountain with elevation 808.5 also belong to this same stratigraphic level, although the comp—

^1 This same genus was named Paleolenus by L. N. Repina.
^2 The Bogoyul Formation corresponds, in our scheme, to the level of the Azyrtal Formation.

Table 1

List of trilobites from the Obruchev, Azyrtal, and Suyaryk complexes

* Not from our collections.

Continuation of Table 1

Table 2

Summary table of the generic and species composition of trilobites of the Obruchevka, Azyrtal, and Suyaryk complexes

Note to Table 1

(List of localities with trilobites of the Obruchev, Azyrtal, and Suyaryk complexes)

1. Sukhie Solontsy. Mountain with elev. 803.5. Usinskaya Formation—Obruchev complex (pts. 1554—1558—1559) [1, 6].
2. Area of the V. Erba River, Dolgii Mys ridge, Usinskaya Formation, Obruchev complex (pt. 529, A—86) [4].
3. Same place, western foot of Mt. Ostraya, Yulinskaya Formation, lower subformation, Azyrtal complex (pt. 1107 and others).
4. Same place, Mt. Ostraya, western and southern spurs, Yulinskaya Formation, lower subformation; Azyrtal complex (pts. 862, 870, 820, 1159) [4].
5. Sukhie Solontsy, area of the mountain with elev. 803.5. Lower subformation of the Azyrtal Formation. Stratotype of the Azyrtal complex (pts. 1548—1543) [6].
6. Same place, from limestone lenses (pts. 606, 609).
7. Sukhaya Erba River, left bank in the closure of the Sukho-Erbinskaya anticlinal fold. Limestones of the lower subformation of the Yulinskaya Formation with the Azyrtal trilobite complex (pts. 625—628, Fig. 1).
8. Right bank of the Sukhaya Erba River, archaeocyathid–trilobite limestones of Mt. Arkheotsiatovaya, mountain with elev. 667.5 and others. Azyrtal faunal complex (pts. Dv 254, 1, K-116, 618 and others, Fig. 2).
9. Area of the village of Katonshkino. Northwestern limb of the Katonshkino syncline. Light-gray massive and dark-gray platy limestones of the so-called Boroyulskaya Formation. Azyrtal faunal complex (collections of A. F. Senyukovets). Lists of fauna according to determinations by I. I. Koptev and A. K. Semyashko [7].
10. Mt. Batykhtag, toward the north of the Ulug-Yol stream. Light-gray massive limestones. Azyrtal faunal complex. Collections and determinations by A. K. Semyashko [8].
11. List of trilobites from the Azyrtal Formation for the Azyrtal complex according to M. K. Vinkman (Sukhie Solontsy, pts. 604, 605) [2].
12. Mt. Arkheotsiatovaya. Northern foot. Archaeocyathid–trilobite limestones (pt. 103/IV) (Fig. 2).
13. Sukhie Solontsy. Mountain with elev. 726.1. Upper subformation of the Azyrtal Formation. Suyaryk complex (pts. 1501—1503, 15, 16, 22, 23).
14. Same place. According to M. K. Vinkman and others, these same beds are assigned to the Karasuk Formation (pts. 620, 641—643) [2].
15. Left bank of the Sukhaya Erba River. Upper subformation of the Yulinskaya Formation. Suyaryk complex (pts. 631—633, 685) (Fig. 1).
16. Mt. Batykhtag. Upper limestone member. Collections and determinations by A. K. Semyashko. Suyaryk complex [8].
17. Mountain with elev. 687.5. Thin-platy limestones with oryctocephalids. Suyaryk complex (Fig. 2).

In Table 1 are placed lists of trilobites from the localities indicated here, and in Table No. 2 are given summary lists for the Obruchev, Azyrtal, and Suyaryk horizons*.

The trilobite complex is not entirely unambiguous in relation to what was said above.

A more complete section for deposits at the level of the Azyrtal, Suyaryk, and higher horizons can be seen on the left and right banks of the Sukhaya Erba River. On the left bank of the Sukhaya Erba River, in the closure of the Sukho-Erbinskaya anticline, first mapped by us jointly with R. B. and N. I. Karpinskii in 1958, a large complex of archaeocyaths (determinations by A. G. Pospelov) and trilobites, determined by us, was collected at that time in light-colored massive archaeocyathid–trilobite limestones of the lower subformation of the Yulinskaya Formation. In our earlier works this complex was called by us the Obruchev complex [7], whereas in the present article, after additional collections and analysis of other materials, it is termed Azyrtal (Table 2).

In deposits lying stratigraphically higher in the northern and eastern limbs of the same anticlinal fold (pts. 631, 633, 685), in light-colored massive limestones almost indistinguishable from those lying below, we at that time collected and determined a trilobite complex called Suyaryk. The composition of the fauna in these beds, as also in

* Localities for which there are no references to other authors belong to us.

stratotype of this complex, is characterized by a sharp predominance of Middle Cambrian genera and species, such as Chondranomocare, cf. plana Roman., Kootenia elongata Rasseti var. ornata Ivschin, Chondragraulos minussensis Lerm., and others.

Here, too, on the southern limb of the Sukhoi Erba anticline, in archaeocyathid-trilobite limestones with the Azyrtal faunal complex, in unclear relations with them and, apparently, unconformably, in loose limestones of light-beige color, we collected and identified the so-called Sukhoi Erba trilobite complex, which is characterized by very good preservation and a very diverse generic and species composition. The complete list of these, in almost each of the known localities, contains numerous species of Middle Cambrian genera, and in the full list of them, published by us for the first time, occur: Pachiaspis typicalis, Res., P. elongatus Tomaschp., Kootenia gaspensis Ras., Kootenia billingsi Ras., Chondranomocare bidjensis Polet., Ch. bidjensis Polet. var. denormis Tomaschp., Olenoides placitus Tomaschp., Olenoides optimus Lazar., Olenoides courtecei Walc., Solenopleura flexibilis Tomaschp., Prohedinella erbiensis Sivov., Gaphuraspis kalievi Ivsch., and other species. Erbia sibirica (Schm.), Chondragraulos minussensis Lerm., and others.

It is very curious that, both on the right and on the left sides of the Sukhoi Erba River, beds with the Sukhoi Erba trilobite complex occur and, apparently, unconformably overlie the archaeocyathid-trilobite limestones with the Azyrtal complex; in some sections they are separated from the latter by a packet of dark-coffee thin-platy limestones, in which, on the mountain with elevation 687.5, and also on Mt. Ostraia, we collected and identified oryctocephalids: Paraoryctocephalops and Oryctocarella. Similar packets of thin-platy limestones had long been known to us in the area of development of archaeocyathid-trilobite limestones between Mt. Arkheotsiatovaia and the Karasuk mine, but for a long time we did not attach significance to them, since no faunal remains had been found in them. The discovery of similar platy limestones^4 at a level below the beds with the Sukhoi Erba complex on Mt. Tas’kynaia (area of the Karasuk mine) attracts our attention because some geologists are trying to place these limestones at the level of the Sladkokornevskaya Formation, within which the presence of numerous packets of dark-coffee and coffee-black platy limestones is indeed known; however, as will be shown below, such a decision is in no way justified.

Of great importance for resolving the question of the stratigraphic position of the thin-platy limestones with oryctocephalids was detailed mapping in the area of Mt. Ostraia during recent years. As is known, as early as 1958, together with R. B. and N. I. Karpinskii, we first collected and identified on the Bateniev Ridge new genera of the family Oryctocephalidae: Paraoryctocephalops and Oryctocarella.

In these works of ours [6, 7, 8], packets of thin-platy dark-coffee limestones with the above-named trilobites were depicted as interbeds in the effusive-carbonate-terrigenous sequence of Mt. Ostraia, corresponding to the level of the lower subformation of the Yulinskaya Formation and the Azyrtal horizon; accordingly, the age of this entire sequence, and consequently of the Azyrtal faunal complex, was determined as Middle Cambrian.

The result of the latest investigations is the confidently established occurrence of thin-platy limestones in troughs of small synclinal folds on the deposits of the Mt. Ostraia sequence, and consequently—

^3 R. T. Bognibova did not participate in these works at that time, and the known lists of trilobites from these deposits were compiled by us.
In all other faunal lists compiled by us from our collections, as well as by R. T. Bognibova from our joint collections (1965), she identified them only as Kootenia.
^4 No fauna has been found in them.

but also the complete identity of this level in different parts of the Batenyov Range. Thus, the stratigraphic position of the thin-platy limestones with oryctocephalids, as it appears to us, should be placed at the level of the Suyaryk horizon, with an age corresponding to the very base of the Middle Cambrian.

From everything set forth above, one may also, with complete obviousness and confidence, draw the conclusion that in the sections of both the left and the right banks of the Sukhaya Yerba River, such horizons as the Azyrtal, Suyaryk, and Sukhoerba can be distinguished quite unambiguously. For the time being we do not touch upon the younger subdivisions.

The materials cited above on the presence of beds with the Sukhoerba trilobite complex, identical down to the species level, in the deposits of both the right and left banks of the Sukhaya Yerba River, and moreover in beds that spatially and geologically overlie archaeocyathid–trilobite limestones that likewise, apparently, belong to a single stratigraphic subdivision—the Azyrtal—had long been known to us from R. T. Bognibova; however, this did not prevent her, in the same section, from distinguishing two archaeocyathid–trilobite horizons: a lower one, or Bed III, with the “Obruchev” complex, and an upper one, or Bed V, with the “Blagodat” complex. The intervening Bed IV, assigned by R. T. Bognibova to the Suyaryk horizon, is composed of trilobite limestones of Middle Cambrian age, to which she refers the light-colored limestones of Mount Tasykhina and the dark coffee-colored limestones making up the western spurs of Mount Arkheotsiatova. To this it should be added that R. T. Bognibova includes in Bed V also the massive light coffee-colored limestones of elevation 667.5 with trilobites, which we call Sukhoerba, as well as the platy limestones with oryctocephalids underlying these limestones.

As shown in Table 2, the composition of the trilobites from Bed III, which corresponds to the position of the archaeocyathid–trilobite limestones in the closure of the Sukhoerba anticline on the left bank of the Sukhaya Yerba River, and the composition of the trilobites from Bed V, which corresponds to the limestones of Mount Arkheotsiatova and the mountain with elevation 667.5, differ in no essential respect and are characterized by those forms that are typical of the stratotype of the Azyrtal horizon. It should be noted that in the limestones of Mount Arkheotsiatova and the mountain with elevation 667.5, near the base of the overlying Sukhoerba limestones, there are unquestionably Middle Cambrian genera: Olenoides sp., Solenopleura sp., Chondranomocare sp.; however, their number is very limited, they occur sporadically, are more often indeterminable to species, and do not change the general composition of the assemblage. The same may be said with regard to the composition of the archaeocyathid beds. As for the composition of R. T. Bognibova’s Bed V, in which she indicates the presence of Middle Cambrian trilobites and which she places at the level of the Suyaryk horizon—in the same deposits we have established three faunal complexes: the Sukhoerba complex in the light-colored limestones of Mount Tasykhina, the Suyaryk complex in the underlying beds, and, as for the dark coffee-colored limestones of the western slope of Mount Arkheotsiatova, here we, as well as many other geologists, depict the western limb of an anticlinal fold composed of the lower beds of the Sladkokorenevskaya Formation. Over a number of years the question of the age of the limestone unit on the western slope of Mount Arkheotsiatova was discussed repeatedly, since the contacts with adjacent units are tectonic. The Sladkokorenevskaya age of these limestones is resolved much more confidently on the basis of the assemblage of trilobites contained in them. Common forms for the limestones of the Sladkokorenevskaya Formation of the western and eastern limbs of the anticline, in the closure of which the limestones of Mount Arkheotsiatova are located, are the numerous species of the genus Antagmopleura, new species of the genus Erbia: Erbia mirabilis Tomascph., representatives of the genus Bathynotus, and also numerous species of the genus Ole-

noides, Giaphuraspis, Chondragraulos, isolated representatives of the genera Kootenia, Kooteniella, which passed over from the Sukhoyerba Formation.

For the deposits of the Sladkokornevskaya Formation on both limbs of the same fold, the absence of forms characteristic of the Sukhoyerba complex is typical. These same deposits on the eastern limb of the fold, where their position is beyond doubt to anyone, were described by R. T. Bognibova under the name of the VI member [1]. We take this opportunity to note that in the list of fauna from these beds, in addition to forms that are indeed characteristic of them, R. T. Bognibova indicates (with a reference supposedly to our determinations) such forms as several species of the genus Pachiaspis, as well as Kootenia gaspensis Ras., K. billingsi Ras., Chondranomocare bidjensis var. denormis Tomasp., and other species, which nowhere and never in this complex were determined by us and which are characteristic only of the Sukhoyerba horizon.

As evidence that the Sladkokornevskaya Formation is exposed on the western spur of Mt. Archeocyatova and that the occurrence of this unit beneath the archeocyathid limestones is in no way proven, we allow ourselves to cite some factual materials. Thus, on the left bank of the Sukhaia Erba River, directly on the limestones with the Sukhoyerba trilobite complex, there lie coarse-platy algal limestones, and still higher—dark-coffee-colored limestones with Amgaspidella (loc. 652), which apparently correspond to the Sladkokornevskaya Formation (figs. 1, 2).

The same relationships are visible on the right side of the river, where, on archeocyathid-trilobite limestones forming a single whole with the massif of Mt. Archeocyatova and Mt. with elev. 667.5, there lie light beige limestones with trilobites of the Sukhoyerba horizon (loc. 1685); higher parts of the section are absent here. However, somewhat farther north at the foot of the western spur of Mt. Archeocyatova it is clearly visible that upon similar algal limestones lie dark-coffee-colored trilobite limestones of the Sladkokornevskaya Formation, and that the contact with the limestones of Mt. Archeocyatova is tectonic. Here too, at the foot of the western slope of the mountain itself, and also at the northern foot, in archeocyathid-trilobite limestones with the Azyrtal complex (locs. 103/IV, 251/III), there occur trilobite biostromes in which forms characteristic of the Sukhoyerba complex are already present, which indicates the existence of a close connection, both spatial and geological, between these complexes.

From all that has been set forth above, we consider it possible to draw the following conclusions.

1. The Obruchev trilobite forms, which appeared in Sanashtykol time (as we have repeatedly emphasized earlier as well), reach their flourishing in Azyrtal time and almost completely die out by Suyaryk time.

2. The peculiarity of the Azyrtal complex consists in the fact that all Obruchev forms that lived in the upper parts of the Usa Formation pass into it, and Solontsovka forms and some Middle Cambrian genera appear. This complex is sometimes difficult to distinguish from the Obruchev proper in the absence of continuous sections, and therefore the interpretation of these complexes during mapping may be very different. Because of the presence in them of many common forms, we propose to call this subdivision the Obruchevian stage. We consider it most correct to determine the age of this subdivision as the upper Lower Cambrian and transitional from the Lower to the Middle Cambrian, for if the base of the Middle Cambrian is drawn at the base of the Obruchev horizon and by the appearance of isolated Middle Cambrian genera, as we did earlier [7], and as many others do, then it must be lowered to the level of the Sanashtykol horizon, where Middle Cambrian genera already appear.

Fig. 1. Schematic geological map of the area of Mount Sladkie Korni. Legend. 1. Light-gray massive limestones with the azyrtal faunal complex. Yudina Formation, lower subformation. 2. Light-gray massive limestones with trilobites of the Suyaryk horizon. Yudina Formation, upper subformation. 2a. Thin-bedded dark limestones with oryctocephalids of the Suyaryk horizon. Yudina Formation, upper subformation. 3. Light-beige limestones with the Sukhorbinka complex. 4. Dark coffee-colored limestones of the Sladkokoren Formation. 5. Archaeocyaths. 6. Trilobites. 7. Oryctocephalids. 8. Fauna-collection localities. 9. Unconformity surfaces. 10. Tectonic contacts.

Fig. 2. Schematic geological plan of the hill with elevation 667.5. The legend is the same as for Fig. 1.

1. At the base of the beds with the Suyaryk complex, or more precisely, with the appearance of beds containing oryctocephalids Paraoryctocephalops and others, the lower boundary of the Middle Cambrian should be drawn, since by this time archaeocyathids and all forms characteristic of the Obruchev and Solontsy complexes almost completely disappear.

2. The convincingly established almost complete identity in the composition of archaeocyathids and trilobites of the “III and V members” of the section of the Karasuk Formation (according to R. T. Bognibova), as well as other geological materials cited for the characterization of the section in the area of Mt. Sladkie Korenya, indicate that both these members are of the same age and, consequently, the sections of the right and left limbs do not build upon one another, and in each of them the same subdivisions are distinguished: the Azyrtal, Suyaryk, and Sukhoerba horizons.

The first two horizons characterize the deposits of the Yulian Formation, while the third complex belongs to the lower part of the overlying Sladkokornev Formation (Figs. 1, 2). The references given by R. T. Bognibova to our general observations on the occurrence of trilobite limestones on the western spur of the hill with elevation 667.5 (here we established the Sukhoerba complex) beneath beds with archaeocyathids in the hinges of small anticlinal folds, as it seems to us, cannot serve as proof of the existence of a second archaeocyathid horizon, or the so-called V member, since all other materials contradict this.

As can be seen from Table 3 appended to the present article, where the stratigraphic subdivision is given for the pre-Devonian deposits of the Batenev Ridge and the Azyrtal Range, we have somewhat modified—or rather refined—our previous views and offer them for discussion by the geological community.

Table 3

Biostratigraphic scheme of the deposits of the Batken Range and the Azyrtal Range
Compiled by V. D. Tomashpolskaya

References

1. R. T. Bognibova. Stratigraphic position and age of archaeocyathid-trilobite limestones in the area of Mt. Arkheotsiatovaya and Mt. Sladkie Korenya of the Batenev Ridge. Proceedings of SNIIGGiMS, issue 34, 1965.

2. R. T. Bognibova, I. I. Koptev, A. G. Sivov, N. P. Suvorova, V. D. Tomashpolskaya, A. P. Shcheglov. On the lower boundary of the Middle Cambrian of Central Siberia. — In: Stratigraphy of the Precambrian and Cambrian of Siberia. Krasnoyarsk Book Publishing House, 1967.

3. M. K. Vinkman, A. V. Ginzinger. Principal types of sections of Lower–Middle Cambrian deposits in the western part of the Altai–Sayan region. Geology and Geophysics, Siberian Branch of the Academy of Sciences, No. 7, 1970.

4. I. I. Koptev, A. K. Semashko, V. A. Shipitsyn. On the question of the age of the massive archaeocyathid limestones of the area of the village of Katushkina (Batenev Ridge). Izvestia TPI, vol. 166, Tomsk, 1969.

5. A. K. Semashko, V. A. Shipitsyn. On the biostratigraphy of Cambrian deposits in the area of Mount Balykhtar (Batenev Ridge). Izvestia TPI, vol. 166, 1969.

6. A. G. Sivov, V. D. Tomashpolskaya. On the question of the stratigraphic position and age of the Elan and Obruchev horizons. Izvestia TPI, vol. 165, 1969.

7. V. D. Tomashpolskaya, R. B. Karpinsky. On the discovery of Middle Cambrian trilobites in the area of the village of Sukhaya Erba (Batenev Ridge). Izvestia TPI, vol. 120, 1961 (1962).

8. V. D. Tomashpolskaya. Stratigraphy and paleontology of the Cambrian of the Batenev Ridge and the Azyrtal Range. Author’s abstract of dissertation. Tomsk, 1964.