GENERAL GEOCHEMICAL FEATURES OF THE INTRUSIVE–VOLCANOGENIC FORMATIONS OF THE TALANOVSKY GRABEN (KUZNETSK ALATAU)

V. Z. Mustafin

(Presented by Professor A. M. Kuzmin)

The Talanovsky graben, located in the northwestern spurs of the Kuznetsk Alatau, is made up of a complex assemblage of volcanogenic formations [11], previously combined into the Telbes series of the Lower–Middle Devonian. Study of the geological structure of the graben has enabled us to distinguish within it three intrusive–volcanogenic formations (from bottom to top): (a) trachyandesite, (b) basalt–andesite, and (c) a formation of intrusive post–Middle Devonian granosyenites. The formations distinguished are characterized by a varied petrographic composition and by a complex internal structure, being composed of various, including subintrusive, facies varieties of rocks [10].

Increasing attention has recently been paid to questions of the distribution of trace elements in igneous rocks. Of particular interest in this regard are collections of articles by groups of authors published in our country [4, 5, 9]. Among the works of foreign researchers, the most important are the series of review articles by the well-known English geochemists C. R. Nockolds and R. Allen [12]. However, as G. I. Rossman [13] notes, there are still few data on the contents of ore-forming elements and their satellites and on the influence of geological factors on their distribution in effusive rocks.

In addressing, to one degree or another, the problem under consideration, many researchers [8, 14, 17] acknowledge that even questions of its terminology remain debatable. Without dwelling on the details of the discussion, we shall merely point out that, in our opinion, it is expedient to use the terminology of V. S. Koptev-Dvornikov and M. G. Rub [8], although it has not been definitively developed. These researchers distinguish between “general geochemical specialization” and “local specialization.”

By general geochemical specialization they understand those features of the behavior of trace elements in rocks in which their average contents exceed Clarke values. In speaking of local specialization, these authors have in mind geochemical (metallogenic) specialization within individual areas (volumes) of rocks. Thus, the concept of local specialization coincides with the concept of the presence of primary halos of dispersion. The concept of metallogenic specialization is a special case of geochemical specialization, and this term should be applied when

the matter concerns specialization of metallic components in ore deposits. In our article, features of local specialization are not considered.

The geochemical features of magmatic formations developed over the area of the Talanovsky graben are considered on the basis of processing the results of semiquantitative spectral analysis (about 2000 samples); Li and Rb were not determined in the samples. The uranium content was estimated by Vasil’ev’s method on a FAS-1 luminescence photometer. The geochemical features of the rocks were determined from samples taken from areas not bearing hydrothermal alterations associated with ore formation.

For the elements detected in the rocks of the graben and characterizing the geochemical features of the latter, average contents were determined statistically; within this area these correspond to their geochemical background (gb). For this purpose, for each element in a given rock variety a variation curve of the distribution of samples by classes was constructed—the mode [2,7], whose maximum corresponds to the content value having the greatest frequency of occurrence in the rocks of the area. This value is least affected by random fluctuation of the sample [2, 13].

The values of element contents are compared with the sensitivity of the analysis and with the Clarke values in rocks of the corresponding compositions according to A. P. Vinogradov [3]. The data obtained make it possible to characterize the general geochemical features of the magmatic formations of the graben as follows.

1. Trachyandesite Formation

Effusives of basic composition. The principal representatives of rocks of basic composition are labradorite and labrador-pyroxene porphyries.

Labradorite porphyries, like other rocks of the Talanovsky graben, are characterized by the presence of a large number of reliably recorded elements, and only the contents of some of them (Nb, Yb, Y) decrease to the sensitivity limit of the analysis. A Clarke content is characteristic only of Sr. Pb, Zn, Sn, Ti, Be, Zr, Y, Yb, Ga, Mn, and P are distinguished by contents higher than or nearly equal to the Clarke values for basic effusives; moreover, Y, Pb, Zn, Sn, and P are found approximately only in one-third of the samples. Only Ba is present in an amount noticeably above the Clarke value. Ni, Co, Cr, partly Cu and V are detected comparatively rarely and in concentrations lower than the Clarke values. Mo, Ag, and Th are completely absent from labradorite porphyries. The uranium content is considerably below the Clarke values (0.00007–0.00024%).

In labrador-pyroxene porphyries, the contents of Cu, Zn, Ti, Be, Ga, Sr, Mn, and P, in comparison with their contents in labradorite porphyries, do not fluctuate, whereas the frequency of occurrence of Ni and Co in them increases at concentrations of these elements equal to the Clarke values or even lower. At contents approximately equal to the Clarke values, Sb and P disappear; instead, in rare samples, Ag and Mo appear in amounts somewhat exceeding the Clarke values.

The concentrations of uranium in these rocks vary from 0.00006 to 0.00061%, which is nearly equal to, or sometimes an order of magnitude higher than, its Clarke content in basic varieties.

In the lavas of the rocks described, the number of samples in which the concentrations of Ni, Cu, Mo, Sr, and Cr exceed the Clarke value increases somewhat.

The frequency of detection of Y and Ba in these rocks decreases, and their contents fall to clarke levels.

The data obtained on the geochemical specialization of the basic effusives of the trachyandesite formation are compared with the features of Polynesian effusive series of the basalt–trachyte and basalt–phonolite series [12], whose composition is very close to the rocks of the formation. As, in general, are the basic rocks proper of such series [11], the types described are characterized by the presence of V, Cr, Ti, Mn, Ni, Co, Sr, Ba, Zr, Y, and Ga. In contrast to the basic rocks of Polynesia, Ga is recorded somewhat less often in them, but Cu, Zn, and Pb are recorded, as well as Sn and especially Ba, Y, and Yb. On the whole, in the basic effusives of the formation a complex of elements is revealed that is typical of rocks formed from basic magmas, and a group of elements (Zr, Sr, Ba, Y) characteristic of alkaline magmas is recorded.

Effusives of basic–intermediate composition. Plagioclase–amphibole porphyrites are characterized by clarke contents of Ni, Cu, and V, the latter being rather rare. The contents of Co, Cr, Ti, Zr, Ca, and Mn are equal to or somewhat higher than clarke values; Sr does not reach the clarke content; and Zn, although rare, substantially exceeds the clarke value. Compared with labrador porphyrites, plagioclase–amphibole porphyrites differ in an increased frequency of occurrence of Ni, Co, Sr, and Mn at analogous levels of their contents. At the same detection frequency, the concentrations of Cr increase somewhat in the rocks under consideration, while the contents and frequencies of detection of Y and Be decrease. Such elements as Yb, Th, and P are not detected at all, and the contents of Cu, Zn, V, Zr, Ti, and Ba are completely analogous to their contents in labrador porphyrites. Uranium concentrations in the varieties described are in some cases somewhat lower (0.0001–0.00011%), and in other cases almost twice as high (0.00034%) as its clarke contents in rocks of intermediate composition.

Comparison of the effusives described with similar varieties of the Polynesian series mentioned shows that, like the latter, they are characterized by approximately the same or lower contents of V, Cr, Ti, Mn, Ni, Co, and Ga; the same or higher concentrations of Ba, Sr, and Zr; and significantly lower and rarely detected contents of Y. Be is constantly present in them, whereas it is not recorded at all in Polynesian effusives.

Effusives of alkaline composition. Trachyte porphyries, representing the cover facies of alkaline effusives, are characterized by clarke or higher contents of Ti, Cu, Sn, Nb, Ga, Ba, and Sr; less-than-clarke contents of V, Cr, Ni, and Co; markedly higher-than-clarke concentrations of Mn, Zn, Pb, Mo, Be, Y, and Yb, and partly Zr. At the same time, compared with labrador porphyrites, trachyte porphyries show decreased detection frequencies of Cr, Ni, and Co, with a decrease in the Ni concentration. An increase is noted in the detection frequencies and contents of V, Pb, Zn, Sn, Be, Zr, Y, and Yb. The contents of Ti, Ba, Sr, and Ga remain unchanged. Mo and Nb appear in appreciable amounts, while P disappears entirely.

Lavas of trachyte porphyries, compared with the more crystallized varieties of the same composition, are characterized by an increase in the contents and detection frequencies of Cr, V, Cu, Ni, and Co; by a decrease in these values for Nb and Yb; by the same characteristics as in their crystallized varieties for Ti, Mn, Pb, Zn, Sn, Be, Zr, Ba, Sr, and Ga; and by the disappearance of Mo. U concentrations, estimated by the pearl-luminescence method, are 0.00014–0.00042% and are at the level of clarke contents for the “average composition of the Earth’s crust” and rocks of acidic composition.

Trachyte porphyries of the stocks are characterized, like other subvolcanic varieties of this composition, by a great diversity of the complex of trace elements. They differ from their effusive analogues in that V, Ti, Ni, Pb, Zn, Mo, U, and Yb are constantly and more often present in large amounts in them. At the same concentrations, but less often, Ga is recorded; in lower concentrations—Y, and more often, and at the same concentrations—Cr. In comparison with the effusive equivalents, the appearance in these varieties of new elements is of interest. Among these, concentrations below clarke values are characteristic of W and Ce, which are reliably recorded. The clarke contents are exceeded by Ag and Cd, as well as by Bi, In, Nb, La, As, Sb, and P.

The orthophyres of the stocks, in comparison with the trachyte porphyries of the stocks, differ in that in them Cr, Ni, Co, Cu, Sr, Ba, and Y either appear or samples with higher concentrations are noted more often. V, Mn, Zr, and Ga are constantly established, but in somewhat lower concentrations, and for the latter the frequency of occurrence increases. Zn, Mo, P, W, Bi, Sn, As, Sb, Ag, Cd, Ta, Nb, La, Yb, Ge, and In are detected in approximately the same concentrations, but noticeably less often. Pb occurs less often and its concentrations decrease. Be is present constantly, but in lower concentrations. Ti and Ce remain without any changes. The concentrations of U, recorded continuously on a luminescence photometer, substantially exceed its clarke for acid rocks. These contents are 2–3 times higher than in the effusive analogues of the same composition.

The geochemical features of the alkaline quartz-free syenites are almost entirely analogous to the features of the stock trachyte porphyries. Unlike the latter, only Mo, Nb, La, Y, and Sr are noted in them in somewhat lower concentrations and less often, while the contents of V, Ti, Ni, and Zr, with their constant detection, decrease somewhat. The concentrations of U and Th in the quartz-free syenites are generally analogous to their contents in the subvolcanic varieties of other alkaline rocks, but sometimes increase for both one element and the other.

Comparison of the geochemical features of the alkaline formations of the graben with the geochemical features of the Polynesian alkaline series of the basalt–trachyte and alkaline basalt–phonolite series shows that both the former and the latter are characterized by complexes of trace elements that are rather diverse in composition. In the alkaline formations of the graben, Cr, Co, Ni, Cu, Zn, and Mo are constantly present, which are absent or not always established in the rocks of Polynesia. In addition, V, Pb, Zr, and Y, which are also typical of the Polynesian alkaline series, are determined in them. In comparison with the latter, La, Ba, and Ca are not recorded in them. These and some other elements (Nb, As, Be, and Sn) appear in areas of local specialization.

The values of the geochemical backgrounds of elements constantly detected in the alkaline rocks of the graben (Table 1) are more or less comparable with their contents in the effusions of Polynesia. Only the contents of Y are one and a half to two times lower, and those of Zr one to two orders of magnitude lower, than in the Polynesian varieties.

The main geochemical features of the formation are expressed in the fact that Ba, Zn, Pb, Zr, Mo, Y, and Nb are constant in its rocks, a complex of which is typical of alkaline series. In addition, Cr, V, Ti, Ni, and Co are constantly detected in them, apparently indicating the basaltic composition of the parental magma.

The least sensitive to changes in the composition of the differentiating magma during the formation of the trachyandesite formation are—

Table 1

Geochemical forms of trace elements in rocks of the intrusive–volcanogenic formations of the Talanovsky graben

are Zn, Pb, and Zr, present in clarke amounts for rocks of the corresponding composition (3), or in nearly clarke amounts. During differentiation, Cu, Ni, and Co—remaining at the level of clarke contents and decreasing only slightly from basic rocks to alkaline ones—change very little. The V content decreases especially sharply in this case (clarke in basic rocks and three times lower than clarke in alkaline rocks). Y concentrations (3–5 times higher than the clarke in basic rocks and falling to clarke values in alkaline rocks) are characterized by a decrease in the course of differentiation. The contents of U and Mo, which for the most part exceed the clarke by a factor of 2–5 in the corresponding varieties, are distinguished by a steady increase from basic products to alkaline ones. In the alkaline varieties, in addition, an increase is observed in the frequency of detection of Sn, Be, Y, Yb, and the appearance of Nb.

II. Basalt-andesite formation

The rocks of the terrigenous-sedimentary sequence constituting the base of the formation are characterized by compositions and contents of trace elements typical of the basic and alkaline effusive rocks of the formation described above.

Basalts, as well as the related and nearly contemporaneous pyroxene-plagioclase (andesitic) porphyrites, are characterized by clarke contents of V, Co, Cu, and Cr. The concentrations of Pb, Zn, Be, and partly V, Mn, Cr, Ba, and Ga are always above clarke. In comparison with the basic effusive rocks of the trachyandesite formation, the rocks under consideration have the following differences: in them, the frequencies of occurrence and concentrations of V, Cr, Ni, Co, Pb, and Sn increase, whereas the contents of Zn and Sr decrease; the contents of Y and Yb decrease sharply; Nb and P disappear completely; and Mn, Ti, Cu, Be, Ba, Sr, and Ga remain unchanged. In these rocks Th is not recorded, while U contents in basalt porphyrites range from 0.00004 to 0.00006%, sometimes rising to 0.00009%. In pyroxene-plagioclase porphyrites the concentrations of U are almost analogous, varying from 0.00006 to 0.00008% and amounting, not infrequently, to 0.00012–0.00018 and even 0.00022%. These values are, in general, approximately equal to the clarke contents of uranium for rocks of basic and intermediate composition.

Comparison of the geochemical features of the effusive rocks of the basalt-andesite formation with the features of rocks of the basalt-trachyte series of the Hawaiian Islands [12] shows that the geochemical backgrounds of elements in the rocks of the graben are more or less comparable for V, Cr, Ti, Mn, Co, and Ni, and also partly for Ba, Y, and Ga, which are more or less consistently detected in the rocks of the Hawaiian Islands as well. Elements such as Pb and Mo, consistently recorded in the rocks of the graben, are absent or occur rarely in rocks of the Hawaiian series. The concentrations of Sr and Zr in the latter exceed by an order of magnitude their contents in varieties of the basalt-andesite formation of the graben, whereas La in both rock series is not always detected. In the rocks of the graben, P, which is consistently detected in the rocks of the series being compared, is often absent.

The composition of the rocks of the basalt-andesite formation is characterized by a comparative closeness of chemistry. The behavior of trace elements during its formation underwent only slight changes. Pb concentrations undergo no fluctuations at all; Ni, V, Cu, Zr, Co, and Zn change very little. U and Mo undergo slight changes; the latter appears only in intermediate varieties.

In general, the geochemical features of the formation amount to the following: a) in terms of the content of trace elements, the rocks of the terrigenous-sedimentary sequence of its lower part are especially similar to the labradorite porphyrites and trachyte porphyries of the trachyandesite formation, the denudation of which led to their formation; and b) according to this feature, the rocks of the basalt-andesite formation are very close to the basic and intermediate effusives composing the lower half of the section of the trachyandesite formation.

III. Formation of intrusive post-Middle Devonian granosyenites

The formation includes rocks of different petrographic composition, occurring in subvolcanic facies.

The intrusive granosyenites, dike syenite-porphyries, and microsyenites are characterized by the fact that the concentrations of Mn, Co, Zn, Cd, Mo, Zr, As, W, Sb, Be, Ag, Ta, and in part Nb, Y, Ga, Ge, Bi, determined in these rocks constantly or almost constantly, substantially exceed A. P. Vinogradov’s clarke values for acidic rocks. The contents of V, Cr, Ti, Ni, as well as Ce, La, Sr, and P, do not reach the clarke values for acidic varieties. The concentrations of Cu, Sn, Ba, and Ti are approximately at the level of the clarke values. The contents of U, measured with a luminescence photometer, are estimated at 0.00006%, which is three times lower than the clarke values for rocks of acidic composition.

Granosyenites are generally characterized by the same assemblage of trace elements as the quartz-free syenites of the trachyandesite formation. Unlike the latter, V, Mn, Co, Cu, Pb, Ba, Zr, Nb, and Mo are detected in them less often or almost constantly, but in lower concentrations. At the same or somewhat lower contents, the frequency of detection of Sr, Sn, as well as In, As, Sb, Ag, U, Th, and P remains the same or increases somewhat, with some of them being recorded constantly. Bi is found more often, though not always, in the same concentrations. Y is established almost constantly, but in higher concentrations. The behavior of the other trace elements in these rocks does not differ in any way from their character in the alkaline syenites of the trachyandesite formation.

The diorite porphyries of the dikes differ from the granosyenites in that the concentrations of the constantly detected V, Mn, Co, Ni, Cu, Zn, Sr, and Ba increase somewhat in them. Pb and, in part, Sn, Be, Zr, Nb, Y, and Yb are found almost with the same frequency, constantly, but in slightly lower concentrations. W, Bi, As, Sb, and Ag are detected at the same concentrations, but more rarely. Ti, Cr, and Mo are recorded with approximately the same frequency, or even constantly, in higher concentrations. Ga and Ge are detected at the same contents, but somewhat more often. The nonconstantly detected Cd, Ta, La, Ce, In, U, Th, and P remain with the former frequency and the same concentrations.

The spessartites included in the described formation, in their geochemical features, are extremely close to the above-described diorite porphyries. The slight difference amounts to the fact that in the spessartites the concentrations of the constantly detected Cr, Ti, Mn, Ni, and Cu, and partly of Sr, which is not always recorded, decrease somewhat. The concentrations of Pb, Ag, Sn, Be, Ba, Y, Yb, and Ga increase somewhat. Ta and Ge are detected somewhat more rarely in the same concentrations.

Table 1 gives the values of the geochemical backgrounds of some trace elements, determined in the graben in rocks of the formation of post-Middle Devonian granosyenites as constant. The absence in the litera-

on the type of effusive and subvolcanic formations, the available data on their geochemical features do not permit a satisfactory comparison of the rocks of the formation described with any definite type.

The behavior of trace elements in the principal petrographic varieties of the formation is characterized by constancy in the concentrations of Zr, Pb, and Li. The contents of V, Ni, Co, and Zr increase from acid varieties to basic–intermediate ones. The concentrations of Y and Mo, however, decrease from acid rocks to basic ones.

In general, all rock types of the formation described are characterized by a complex assemblage of trace elements, since its formations occur exclusively in subvolcanic facies; moreover, in terms of geochemical features they are quite clearly subdivided into acid- and intermediate-composition varieties.

IV. Carrier minerals and concentrator minerals of trace elements

The formations described consist predominantly of volcanogenic varieties of not very high recrystallization, which ruled out the possibility of separating monomineralic fractions. Therefore, in order to clarify the question of carrier minerals and concentrator minerals [15] in the rocks of the formations, only artificial concentrates were studied, obtained from samples weighing 6–8 kg from rocks of subvolcanic facies of various composition; their number was about 40.

Analyzing the results obtained, one may conclude that the carrier minerals in the rocks of dike and intrusive bodies of various composition are ferromagnesian aluminosilicates (amphiboles, pyroxenes), as well as feldspars.

In pyroxenes and amphiboles, the magnitudes of concentrations and the frequency of occurrence of trace elements differ somewhat. Only Mn, Ti (0.5–0.08%, and sometimes 0.2%), and Cu (0.001–0.008%) are determined in them constantly and with identical contents. Cr (up to 0.008%) and also V are found almost constantly both in pyroxenes and in amphiboles, but in pyroxenes its concentrations amount to as much as 0.008%, whereas in amphiboles they are no more than 0.002%. In both, Ni (0.001–0.008%) is often present, and in isolated cases Co (0.001–0.005%) and Zr (0.001–0.002%) are noted. In pyroxenes constantly, and in amphiboles in isolated cases, Ba (0.001–0.002%) and Sr (0.001–0.008%) are recorded. In amphiboles Y is also sometimes present (0.002–0.005%).

Pb and U are detected in potassium feldspars. In addition, other rare elements—In, Ga, and Ge—may be concentrated in them [1, 6]. Plagioclases and nepheline, which play the role of rock-forming minerals in the graben rocks, may contain elevated concentrations of Ge and especially Ga (0.0096–0.0020%), and biotites may contain In, Ge, Ga, and Cd.

The concentrator minerals in the rocks of the intrusive-volcanogenic formations of the graben, regardless of their composition, form the following series in degree of abundance: magnetite, zircon, apatite, grossular, ilmenite, pyrite. The assemblage of trace elements in the named accessory minerals is usually complex, and no dependence of its composition or of the concentration values of individual elements on the type of formation is observed.

In magnetite, represented by a titaniferous variety, in addition to high concentrations of Fe and Ti, spectral analysis constantly records

Mn (0.005–0.8%) and Cu (0.001–0.005%) are recorded. Cr (0.001–0.002%), V (0.001–0.005%), and Ni (0.001–0.002%) are usually found; Zr (0.001%), Zn (0.001–0.008%), and Mo (less than 0.001%) are often established. Pb (0.001–0.008%) and Y (0.001–0.005%) are determined somewhat less frequently; in isolated cases Co and Yb (0.001%), as well as Be (0.002%), occur.

The suite of trace elements in zircon is especially diverse, with consistently significant contents of Mg (~1.0%), Mn (0.05%), Ti and Ni (up to 0.008% each). Pb (0.002%) is always found, and Be (0.001–0.008%) and Y (0.001–0.08%) occur in variable concentrations. Fairly high contents of other rare elements are constantly recorded: Yb (0.05%), Ta (0.008–0.02%), and Th (0.5%), as well as relatively low Nb (0.001%). In cyrtolites its amount increases to 0.008–0.8%. In isolated cases Cr (0.001%) is detected. Apatite constantly contains Al and Mn (0.05%), as well as Mg (up to 0.5%), Ti (0.002–0.2%), Sr (0.001–0.002%), and Cu (0.001%).

In grossular, Fe and Mg (up to 1%), Ti (0.002–0.008%), Cu (0.002–0.005%), and Pb (0.002%) are constantly established. Zr (0.005%), Cr, and Sr (0.001%) are not always detected.

The suite of trace elements in sphene is comparatively poor. Al (0.05%), Fe (0.08%), Ti (0.005%), and Cu (0.002%) are almost always recorded in it.

In ilmenite, Al (0.05%), Fe, Ca, Mg (0.8% each), and Cu (0.002%) are constantly found, along with variable amounts of Ti (0.002–0.8%). Sometimes Be (0.001%) is also detected.

Conclusions

1. The suite of trace elements in the rocks of the formations considered is determined chiefly by the features of the petrochemical composition of the latter. In the rocks of the trachyandesite formation, such trace elements as Nb, La, and Mo are constant. In the rocks of the formation of post–Middle Devonian granosyenites, only Nb is determined in amounts close to Clarke values, while the concentrations and frequency of occurrence of La and Mo decrease. These elements are not established at all in the rocks of the basalt-andesite formation.

2. The composition of the trace-element suite in the rocks of the formations depends substantially on their facies characteristics. In subvolcanic varieties, as compared with their effusive types, irrespective of their composition, a much more diverse suite of trace elements is noted; among them appear W, Be, Ag, Cd, Bi, Nb, Ta, La, In, Yb, Ce, and P. The concentrations and frequency of occurrence of Pb, Zn, Zr, Mo, and Y increase noticeably. This feature of subvolcanic facies was already noted by M. A. Usov [16].

3. The concentrator minerals and their trace elements in the graben area, in general, cannot yet serve as one of the indicators characteristic of the distinguished formations; however, the amounts of the same accessory minerals and their external features differ among the rocks of the formations.

LITERATURE

1. Anikeeva N. F. The role of various associations of chemical elements in the geochemical and metallogenic specialization of magmas. In: Metallogenic Specialization of Magmatic Complexes. Nedra, 1964.

2. Beus A. A. et al. A Guide to the Preliminary Mathematical Processing of Geochemical Information in Prospecting Work. Gosgeoltekhizdat, 1966.

1. Vinogradov A. P. Average content of chemical elements in the principal types of igneous rocks of the Earth’s crust. “Geochemistry,” 1962, No. 7.

2. Geology and geochemistry of granitoid rocks. “Nauka,” 1965.

3. Geochemistry of Variscan intrusive complexes of the northern Tien Shan. “Nauka,” 1966.

4. Ivanov V. I. Geochemistry of dispersed elements (Ga, Ge, Cd, In, Tl) in hydrothermal deposits. “Nedra,” 1966.

5. Use of dispersion halos of uranium and associated elements in prospecting for and exploration of hydrothermal uranium deposits (methodological manual). “Nedra,” 1964.

6. Koltev-Dvornikov V. S., Rub M. G. On the geochemical and metallogenic specialization of magmatic complexes. In: “Metallogenic Specialization of Magmatic Complexes.” “Nedra,” 1964.

7. Metallogenic specialization of magmatic complexes. “Nedra,” 1964.

8. Mustafin V. Z. Geological-tectonic structure of the Talanovsky graben (Kuznetsk Alatau). Proceedings of the XVIII Scientific Conference of the Geological Faculty, DVPI, Vladivostok, 1968.

9. Mustafin V. Z., Kryukov V. G., Lykhina N. S. Principal features of the geological structure of the Talanovsky graben (NW slope of the Kuznetsk Alatau). Izvestiya TPI, vol. 151, 1966.

10. Nockolds S. R., Allen R. Geochemical observations. Geochemistry of certain series of igneous rocks. IL, 1958.

11. Rossman G. I. Endogenous geochemical anomalies and their significance for prospecting ore deposits. In: “Application of Geochemical Methods in Metallogenic Studies of Ore Districts.” “Nedra,” 1966.

12. Smorchkov I. E. Determination of the “metallogenic specialization of magma.” In: “Metallogenic Specialization of Magmatic Complexes.” “Nedra,” 1964.

13. Tauson L. V. Geochemistry of rare elements. Publishing House of the Academy of Sciences of the USSR, 1961.

14. Usov M. A. Geology of ore deposits of the West Siberian Territory. Publishing House of ZSGGT, 1953.

15. Shatalov E. T. Review of terms and concepts characterizing magmatism. In: “Review of Geological Concepts and Terms as Applied to Metallogeny.” Publishing House of the Academy of Sciences of the USSR, 1963.