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- Alkali rock dykes d
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Palaeozoic Erathem Being the most important from the economical point of view, rocks of this age compose massifs of two associations: (i) alkali-ultrabasic with carbonatites, and (ii) agpaite. There are a lot of data on these rocks obtained by A.E. Kukharenko, I.V. Bussen, A.S. Sakharov, A.V. Galakhov, S.I. Zak, T.N. Ivanova and many other geologists. These massifs are widely spread in the Kola peninsula and are spatially connected with the Oslo-Khibiny NE-SW trending Zone. The first association (alkali-ultrabasic with carbonatites) includes the Kovdor, Sebl'yavr, Afrikanda, Turiy Cape, Vuorijarvi, Sallanlatva Massifs and some others, the second association includes the huge layered Khibina and Lovozero Massifs. Most massifs are multiphase and are considered to be the ring intrusions; they have a funnel-, lopolith-, laccolith- and stock-like form. Their rocks form three complexes: (i) alkali ultramafic, (ii) nepheline syenitic and (iii) carbonatitic. All the variety of the rocks of the alkali-ultrabasic massifs corresponds to a suite of olivinite-pyroxenite-melilite rock-melteigite-ijolite-nepheline syenite. In general, the massifs are composed of one or several varieties of these rocks. The Lesnaya Varaka and Afrikanda massifs, for instance, are mainly composed of olivinites and pyroxenites; the Sallanlatva and Ozernaya Varaka massifs - of nepheline pyroxenites, melteigites, ijolites and carbonatites. The group under consideration is characterized by carbonatites. The nepheline syenites are presented in the Khibina massif by chibinite, foyaite, lyavochorrite, and rischorrite-juvite complexes of different age. Alkali ultramafites are spread in this massif widely enough [2, 25]. In the Lovozero pluton, mostly spread rocks are foyaites and lujavrites. Carbonatites have been discovered only in the Khibina Massif. All these alkali rocks and the Lovozero group volcanics linked spatially with them, are considered to belong to a single volcano-plutonic association. The ore deposits of apatite, phlogopite, vermiculite, Al, Fe, Ti, rare metals and REE are linked with the massifs of both associations, the Khibina and Lovozero deposits being unique. The development of the Khibina and Lovozero massifs as well as of ultrabasic-alkali intrusives occurred 360-380 Ma ago [71]. Alkali rock dykes d4, pipes of kimberlites, alkali picrites and melano-nephelinites. Along with the ring massifs, the Caledonian alkali magmatism is represented by dyke complexes and explosion pipes. The dykes are located both within the alkali massifs and out of them, they forming swarms out of the intrusions. The swarms have the NE strike, and the dykes are some kilometers long and 50 meters thick. The largest dyke complexes, the Kandalaksha, Prolivy, Por'ya Guba, Mavra Guba ones, are shown in the Map. They consist of alkali picrites, lamprophyres, meymechites, melteigites, nephelinites, alnцites, alkali trachytes, phonolites, carbonatites and some other alkali rocks. In the Khibina massif, along with the dykes of the main intrusive complexes, widely spread are dykes of the final stage of the massif development, with these dykes being mainly composed of alkali picrites and olivine melanephelinites [3]. In the Lovozero massif, dykes are composed of alkali lamprophyres, nepheline basalts, and tinguaites. In the country rocks of the Kovdor massif, dykes consist of alkali picrites, alnцites, phonolites, tinguaite-porphyries and predominant nephelinites. Explosion pipes are known in the Ivanovka Bay area [56], the Khibina massif, the Bol'shaya River area, the Yelovy Island and the Kandalaksha Bay area. In general, by the predominant composition distinguished are three main varieties of the explosion pipes, i.e. kimberlitic (i), alkali picritic (ii) and melanephelinitic (iii). The greatest number of the explosion pipes is established in the Tersky coast eastwards from the Turiy Cape where, according to M.M. Kalinkin, they are conditioned by the Ermakovskiy graben. They are composed of alkali picrites, olivine melitites and ultrabasic foidites. The two last varieties of the rocks compose dymond-bearing kimberlite pipes. The most perspective from the exploration point of view is the area of the narrow entrance in the White Sea [52]. The Kontozero alkali and nepheline syenite massif of the Carboniferous age is situated in the north-western marginal part of the Kontozero caldera. In the massif, along with the predominant syenites established are pyroxenites and melteigites. A thin nepheline syenite body was discovered by drilling in the eastern part of the caldera. The alkali rocks are intrusive into the Lower Carboniferous sedimentary and volcanic rocks. An ultrabasic rock massif is supposed to occur under these sediments and volcanics [35]. MAIN PROBLEMS OF REGIONAL RESEARCHES According to the Note, the main problems of the regional geology result firstly from the lack of reliable data on interrelations between definite geological bodies, their primary position in the supracrustal section of the Kola Precambrian and their origin. It refers, first of all, to high grade metamorphosed and reworked rocks of the Archaean age, in particular, that have lost almost completely their primary features. As a result, it is impossible to stratify these rocks on the lithostratigraphic base. Stratigraphic subdivision becomes possible when we have data on sedimentary and volcanic rocks with primary textures and structures rocks survived in some small domains. These data, however, are not sufficient enough for correct conclusions to be made about a primary succession of any single complex, not speaking about a regional succession. As the Proterozoic formations are considered to be more informative, the main problems are mainly connected here with their regional correlation and a different level of knowledge about separate Lower Proterozoic terranes. The main problem of the intrusive rocks subdivision is in the lack of exact data on a geological (relative) age of many intrusives, especially in zones of both high strain and high grade of metamorphism, and in a small quantity of isotope age determinations. These circumstances causes difficulties in determining a lateral set of magmatic rocks because it has been traditionally made on the base of their petrological features. The most important is a question - do Early Archaean rocks occur in the Kola peninsula or not? Components of these rocks have not been found out yet, and the basement complex shown in the Map presents only the lowest part of the section of the Kola-Belomorian Complex. The heart of the problem is turned only into searching these rocks, with the search being mainly carried out by systematic isotope dating and determining model Rb-Sr and Sm-Nd ages. It is obvious that the discovery of Early Archaean rocks in future will not sufficiently change the outlines of the geological bodies shown at present in the Map but amend our interpretation of the region's evolution. A further subdivision of the Kola-Belomorian complex and getting more specific information about its volume depends greatly on a precise isotope dating taking into account a short time interval of the complex development as a whole. In future, the solution of this problem is possible by recognizing the chronostratigraphic principle as the only possible one to subdivide similar complexes against the lithostratigraphic principle. It should be mentioned here that an isotope dating serves at present as the only method to solve both this problem and most similar ones but only when we have rocks suitable for dating and unambiguous interpretation of their position in a section of geological objects studied. As for the Kola-Belomorian Complex, the top priority task here is the age interrelation between the Chudz-Yavr unit of the central Kola-Norwegian Zone and the Oleny'ya Gora (iron ore-bearing) unit of the near Imandra area. We consider them to be related to one and the same level. These units contain banded iron formations and are characterized by pressure regimes of metamorphism similar to each other, which has allowed to include them into the Kola-Belomorian Complex. At the same time, obvious are differences in the sections of the Chudz-Yavr and Olen'ya Gora units, in their structural pattern and the grade of metamorphism as well as in the content of iron ores. The Olen'ya Gora unit is mainly volcanic in nature; their rocks compose narrow structures between granitogneissic blocks or domes and form a specific lap or oval pattern. They are metamorphosed under conditions only of amphibolite facies and contain the largest economic iron ore deposits. The Chudz-Yavr unit, on the contrary, is of terrigenous lithology, is metamorphosed under granulite facies conditions and contains insignificant iron ore mineralization. Isotopic data available are not sufficient to determine the relations between these two units. The necessity of a precise dating of the Olen'ya Gora volcanics is also conditioned by a great similarity of its section with that of the Lopian stratified terranes of the Kolmozero-Voron'ya Zone the greenstone rocks of which are distinguished by us as younger ones against those of the Chudz-Yavr and Volshpakhk units. Among the urgent problems connected with a further study of the Lopian stratified complexes is the determination of precise ages of volcanic rocks on zircon through all the zones and getting, herewith, convincing data in favour of their higher stratigraphic position against the Kola-Belomorian rocks. Supracrustals spread westwards of Kovdozero Lake have been related also to the Archaean stratified complexes, and this decision is also open to discussion. At present, the volume and area of the Peschanoozerskaya Formation rock spread in the Terskaya Zone are, probably, grossly exaggerated. Compiling the Map, we have taken a version based on the results of a large-scale geological mapping, but this version is not the only one because it is possible that the unit of graded-bedded micaceous and garnet-micaceous schists from the given formation to the analogous rocks of the Vysokaya Zemlya Formation completing the Lopian stratified section in the Terskaya Zone. Lots of unsolved problems of the geology of the Archaean supracrustals are connected with a long-term tendency to map these rocks considering boundaries between separate geological bodies observed at present and being often ambiguous only as stratigraphic as well as with mapping on the base of routs cross the strike of rocks. We believe, the most part of the Archaean rocks should be re-mapped, with real geological bodies being distinguished and followed along their strike. It is obvious that the stratigraphic subdivision of these bodies is possible only in case of their top and bottom to be definitely determined. Debatable problems concerning the stratigraphic boundary between the Upper Archaean and Lower Proterozoic supracrustals may be solved by an isotope dating of suitable Upper Lopian and Sumian rocks. For this purpose we need a single succession consisting of unambiguous Upper Lopian and Sumian formations. The most suitable section is located in the eastern part of the Imandra-Varzuga Zone in the Malye Keivy Ridge area. Strictly speaking, the rocks that are considered there as deposits of the Pestsovaya Tundra Formation (the Snezhnoborskaya Formation) are related to this formation only on the base of their composition, i.e. conditionally, for they are isolated from the stratotypical Pestsovaya Tundra rocks. Only the position of these rocks in the section, their lithology and succession are the basis for such a correlation. But there are some grounds to doubt, so this problem needs to be further investigated. Nevertheless, the attention should be paid to the position of the Pestsovaya Tundra Formation in the eastern part of the zone. The quartzose metasandstone and metagravelstone unit separates here the Sumian section from Archaean granitogneisses and frames the Sumian rock exposures. No effect of the synchronous volcanic activity on these rocks is observed here and they do not interbed or alternate with volcanics at the top and bottom of the unit. The Pestsovaya Tundra Formation rocks are established to lie on the oldest gneisses and granitoids and sometimes on a crust of their weathering. There are no data about a younger Sariolian age of this formation for the Sariolian sections are of another lithology and structure and have a different position in the regional structure. The data available make the authors interpret the position of the Pestsovaya Tundra Formation as an underlying one of the Sumian section and completing the schists section of the Keivy Group, which is related to the Upper Lopian. It is obvious that only additional investigations and isotope age determinations may transfer this problem from hypothetical comparisons to the level of well-grounded solutions. The layered peridotite-pyroxenite-hypersthene gabbro massifs are representative of the Sumian ones according to the age determinations. Products of weathering of these massifs are considered to be found in the Sariolian conglomerates of the Pechenga and Northern Karelia Zones. If it is the case, the emplacement of the massifs should be connected with the Sumian magmatic activity, which contradicts to the data about the multistage magmatic evolution in different zones, i.e. volcanic rock associations of the early stage of the subsidence evolution have been developed in the Pechenga-Varzuga Zone at the Sumian time and in the Northern Karelia Zone - at the Jatulian time [33]. Then the Olanga, Kivakka and Tsipringa massifs also should be of the Jatulian age. But geochronological data contradict this suggestion, so there is nothing to do but to consider that the emplacement of these layered massifs is a result of the Sariolian magmatic activity in the region. It is proved to be correct to relate conglomerates that contain the fragments of the massifs to the Jatulian level rather than to the Sariolian one which they have been traditionally referred to. In basal conglomerates related to the Lower Proterozoic deposits of the Kuusamo area dated were three pebbles of quartz porphyry which are absent in that area but are widely spread through the Pana-Kuolajarvi Zone (northern Karelia). Zircons from all the three pebbles are of 2405+/-6 Ma, which determines the lower age boundary of the Kuusamo rocks, on the one hand, and the Sariolian age of the Pana-Kuolajarvi quartz porphyry, on the other hand [74]. If the layered intrusions that are located in northern Karelia are related to the Sariolian, then it is necessary to consider more thoroughly the vertical set of the intrusive complexes considered by us as post-Sumian. Such data are available, but the consideration of the Sariolian as a higher order stratigraphic unit, re-examination of its volume, structure and interrelations with the Sumian and Jatulian is only being worked out. The Pana-kuolajarvi Zone is unsufficiently studied for it is subdivided by the state border into two parts. Its eastern part adjacent to the border was inaccessible for study, the western part is studied by Finnish geologists up to the border. Such a separate study of the zone resulted in a different interpretation of its structure with opposite versions. Thus, based on the materials available we believe that there is a synclinorium in that area and the youngest Hosijarvi volcanics occur in the synclinorium core. An excursion to the western part of the zone has shown that Finnish colleagues have the grounds to consider this part to be composed of the Salla complex rocks that are the oldest Karelian volcanics there. It means that the central part of the zone may have a dome structure rather than a synclinorium one, with the former being eroded up to the Sovajarvi or Nivajarvi volcanic rocks. The solution of this problem is obvious - a joint study of the zone by Finnish and Russian geologists. Of poor knowledge is the stratigraphy of the Tominga and South Pechenga Groups because their rocks are very poor exposed, are subdivided into blocks by faults, and have a complicated structure, especially in the South Pechenga domain. In spite of a rather sufficient knowledge of the Late Proterozoic sections, they are sometimes difficult to be correlated. One of main reasons is that the sediments deposited under continental and shelf seas conditions differ greatly in lithology, which makes it impossible to confidently use lithostratigraphic methods. There are a few geochronological data. Due to it, one of the most disputable problems concerning with the stratigraphy of the Late Proterozoic of the Kola peninsula will, probably, be the problem of correlation between the sedimentary complexes of the Rybachy and Sredny peninsulas. The solution of it appears to be in a more thorough selection of microphytofossils from the Rybachy peninsula deposits as well as in a study of the geology of the junction zone between these two regions. Of great importance is the problem whether the deposits of the upper part of the section of the Kuyakanskaya and Pumanskaya Formations are related to the Upper Riphean or to the Vendean. A set of microphytofossils determines them to be of the Upper Riphean age but by the nature of the section and some lithostratigraphic features they are similar to the Vendean sediments of the Tanafjord Group (Norway). The correlation of the sediments deposited on the Tersky and Barents Sea coasts of the Kola peninsula is possible at present only by microphytofossil analysis because of these sections being isolated. The problems of the geology of the Early Precambrian intrusive rocks as in case with the supracrustal ones are mainly due to lack of data about the boundaries and lithology of certain massifs and about their isotopic age as well. It is obvious when getting acquainted with materials on the Murmansk block composed mainly only of plutonic rocks. It is this territory that needs to be re-mapped for the first turn based on the principles and isotopic dating mentioned above. Of great difficulty is the subdivision of the Upper Archaean granitoids, the earliest complexes of diorites, tonalites, trondhjemites, granodiorites and enderbites, in particular. The rightfulness of their being distinguished from the most ancient basement should be proved by additional geochronological studies. Parallel to it solved may be the problem of their relative volume; the only difficulty is in great similarity in rock associations of granitoid complexes of different age. Dating is also necessary to prove the distinguishing of two gabbro-anorthosite complexes of different age, i.e. the Upper Archaean and Lower Proterozoic ones. The Lower Proterozoic age of the latter is convincingly proved by age determinations testifying that their emplacement coincides with the development of the layered peridotite-pyroxente-hypersthene gabbro intrusions. It makes us believe that the Main Ridge Massif was formed 40 Ma later than the Monchegora pluton. Taking into consideration the well known data about the similarity in the structure, rock and mineral composition of these two massifs, we may believe in their genetic affinity. In accordance with all said above it should be necessary to date leucogabbro and gabbro-anorthosites of the upper parts of the section of the Panskaya and Fedorova Tundra Massifs. All the rocks mentioned are absent on the present eroded surface in the Monchegora pluton. Unfortunately, we have no reliable geochronological data on alkali rocks of the Jatulian-Kalevian magmatic cycle and on alkali granites associated with the multiphase Gremyakha-Vyrmes Massif. Dating of these granites allows to solve the problem whether it is possible for two groups of alkali granites of different age to be present in the region. Similar thoughts have already been suggested by geologists. In conclusion, we express hope that the generalization of the geological materials on the Kola region as the Map of a scale of 1:500 000 and distinguishing the main problems opens new possibilities for closer co-operation with geologists of the Northern European countries to solve common problems of the regional geology of the Baltic Shield. ЛИТЕРАТУРА REFERENCES 1. Авакян К.Х. Геология и петрология Центрально-Кольской гранулито-гнейсовой области архея. М., 1992. 168 с. Avakyan, K.Kh. Geology and Petrology of the Central Kola Archaean Granulite-Gneiss Area. Moscow, Nauka, 1992. 168 p. (in Russian). 2. Арзамасцев А.А. Щелочные ультрамафиты в Хибинском массиве: новые данные и петрохимические следствия // Щелочной магматизм северо-восточной части Балтийского щита. Апатиты, 1990. С.3-15. Arzamastsev, A.A. Alkali ultramafites in the Khibina Massif: new data and petrochemical consequences // Alkaline Magmatism of the North-Eastern Baltic Shield. Apatity, 1990. P.3-15, (in Russian). 3. 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Evolution of the Kola region, Baltic Shield, Russia: Late Archaean crust in a Palaeoproterozoic craton // EUG VII Strasbourg, France 4-8 April 1993. Terra Nova, 1993, v.5, Abstract supplement No. 1. P.322. П р е п р и н т А.Т. Радченко, В.В.Балаганский, А.А.Басалаев, О.А. Беляев, В.И. Пожиленко, М.К. Радченко ОБЪЯСНИТЕЛЬНАЯ ЗАПИСКА К ГЕОЛОГИЧЕСКОЙ КАРТЕ СЕВЕРО-ВОСТОЧНОЙ ЧАСТИ БАЛТИЙСКОГО ЩИТА МАСШТАБА 1:500000 Технический редактор В.А. Ганичев Подписано к печати 21.12.93. Формат бумаги 60х84 1/16. Бумага офсетная. Печать офсетная. Усл.печ. л. 5.6. уч.-изд.л. 8.22. Усл.краско-от. 5.6. Заказ №57. Тираж 100 экз. _______________________________________________________ Ордена Ленина Кольский научный центр им. С.М. Кирова РАН 184200, Апатиты, Мурманской, Ферсмана, 14. жүктеу/скачать 6.67 Mb. Достарыңызбен бөлісу:
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