UNITED STATES DEPARTMENT OF THE INTERIOR 

GEOLOGICAL SURVEY

The Kola Superdeep Drill Hole by Ye. A. Kozlovskiy (1984):

A detailed summary 

BY

James W. Clarke, Robert C. McDowell, John R. Matzko, Paul P. Hearn, 

Daniel J. Milton, Donald J. Percious, Dorothy B. Vitaliano, and

Gregory Ulmishek

Open File Report 86-517

This report is preliminary and has not been reviewed for conformity with 

U.S. Geological Survey editorial standards and stratigraphic nomenclature,

REPRODUCED FROM BEST AVAILABLE COPY

1986
PREFACE

In 1984 a book was published in the USSR that summarized in detail the 

results of the drilling and scientific studies up to that time of the Kola 

Superdeep Drill Hole on the Kola Peninsula. The bibliographic reference for 

this book is: Kozlovskiy, Ye. A., 1984, Kol'skaya sverkhglubokaya: Moscow, 

"Nedra," 490 p.

The U.S. Geodynamics Committee of the National Academy of Sciences 

asked the Academy's Continental Scientific Drilling Committee for a summary 

of this book. The request was transmitted to the U.S. Geological Survey, 

where the various chapters were summarized by the following persons:

Foreword, p. 4-18, James W. Clarke

General geology, p. 19-65, Robert C. McDowell

Rocks and rock-forming minerals, p. 66-101, John R. Matzko

Geochemistry, p. 102-177, Paul P. Hearn

Mineralization, p. 178-214, Daniel J. Milton

Gases, organic matter, hydrogeology, p. 215-282, Donald J. Percious

Geophysics, p. 283-327, James W. Clarke

Magnetic properties, p. 328-374, Dorothy B. Vitaliano

Drilling, p. 375-480,..Gregory Ulmishek

A full translation of this book is being prepared by Springer Verlag. 

We hope that this review will so stimulate the reader's interest that he will 

avail himself of the opportunity to read the entire book when it is published.

We gratefully acknowledge the assistance of Juanita J. Page of Deep 

Observation and Sampling of the Earth's Continental Crust, Inc. and Teddy A. 

Clevenger of the U.S.G.S. for preparing the copy.

James W. Clarke 

Summary editor
CONTENTS

Page

Foreword 1

General geology 11

Rocks and rock-forming minerals 29

Mineralization 75

Gases, organic matter, hydrogeology 91

Geophysics 137

Magnetic properties 147

Drilling 201

-
ABSTRACT

Drilling of the Kola Superdeep well (SG-3) was begun in May, 1970 on 

the Kola Peninsula above the Arctic Circle in northwestern U.S.S.R. This 

book presents the main results of studies to its present depth of 11,600 m. 

The work is divided into three parts: geology, geophysics, and drilling.

Geology. The area of drill hole SG-3 is underlain by ancient igneometamorphic rocks of the Baltic shield. Archean crystalline basement is 

overlain by Proterozoic metamorphosed sedimentary and volcanic rocks.

The Archean consists of the Kola Series and is divided into two sequences: biotite-plagioclase and biotite-amphibole-plagioclase gneisses 

and amphibolites at the base, and biotite plagioclase and muscovitebiotite-plagioclase gneisses containing high-alumina minerals (sillimanite, 

kyanite, garnet) above.

The Proterozoic in drill hole SG-3 consists of metamorphosed tholeiitic 

metabasalt, metapyroxenite, metaperidotite, metatuffs, and a variety of 

metasedimentary rocks (sandstones, arkoses, carbonates) of the Pechenga 

Complex.

Drill hole SG-3 is located in the Pechenga copper-nickel sulfide 

district. The greatest concentrations of ore minerals were found in 

zones of pyrrhotite mineralization of the Pechenga Complex. Commercialgrade copper-nickel ore was found in the 1665-1830 m depth interval. 

Three types of ores are found in the Pechenga Complex: disseminated ores 

in altered peridotite, breccia ores in disturbed zones, and veinlet and 

disseminated ores in phyllites. Ultramafic intrusives are doubtless the 

source of copper-nickel ores.

The downward increase in temperature of metamorphism is accompanied 

by a transition from brittle to ductile deformation. However, one of the 

unexpected findings was' a wide distribution at all depths of fissures 

with various^ mineral fillings. It was found that mineralized zones of 

crushing, cataclasis, fracturing, and low temperature hydrothermal alteration, including sulfide mineralization, extend to depths 3 or 4 times 

what had been expected.

Gas content of drilling mud and of cores was measured. Anomalous 

high concentrations of all components were detected down to 11,500 m. 

Methane content decreased .with depth from 0.05% in the Proterozoic rocks 

to 0.03-0.01% in the Archean rocks. Helium content tends to increase 

with depth.

Drill hole SG-3 penetrates an ancient Proterozoic artesian basin. 

Gravitational water is distributed throughout the entire section of metamorphic rocks, marking the first time that ground water has been found 

under such conditions. This water is similar to d^_ep metamorphosed marine 

connate water of ancient platforms and intermentane basins.
Ground water in the 0.8-7 km interval is of the sodium-chloride 

composition, salinities increasing with depth and reaching saturation in 

some intervals. Water in the 4.5-9 km interval is not connected 

hydraulically with the overlying zone; the water level immediately rose 

80 m when this zone was penetrated. Below 7 km depth the water becomes 

calcium-chloride and calcium-sodium-chloride type. A constant inflow of 

water was observed during drilling.

Crustal development in the region of drill hole SG-3 was in two 

great cycles: the Archean (older than 2.6 billion years) including two 

stages: 1) sedimentation and volcanism, and 2) folding, metamorphism, and 

ultrametamorphism; and Proterozoic (2.6-1.1 billion years) including four 

stages: 1) subsidence of mobile belt, 2) andesite-basalt volcanism, 3) 

picrite basalt volcanism, and 4) folding and metamorphism.

The Conrad surface was not detected in the drill hole; a migmatitic 

plagioclase gneiss is present where the basaltic layer was expected. A 

continental crust comprising three layers is indicated: granite gneiss 

(0-15 km), granulite gneiss (15-30 km), and a protocrust (30-40 km). Extrapolation of geochemical trends down to 35 km suggests that the protocrust 

was formed from rocks close to sodic dacite in composition.

Geophysics. These investigations included well logging, density and 

porosity-permeability, acoustical properties, electrical properties, magnetic properties, radioactivity, heat flow, and mechanical properties.

The following logs were made in drill hole SG-3: acoustical, laterolog, 

resistivity, spectrometric-gamma, gamma, neutron, impulse neutron-neutron, 

magnetic, electrical potential, spectrometric neutron-gamma, gamma-gamma, 

selective gamma-gamma, thermal properties, caliper, vertical seismic profiling, and gas logs. At a depth of 11 km the variation in the length of 

the cable may be 20 m. This was compensated by adjusting logs to marker 

horizons.

Values of porosity of the Proterozoic meta-igneous and metasedimentary 

rocks are in- the 0.4 to 0.6 percent range, and permeability is in the 0.3 

to 1.2 md range. Archean gneisses have a porosity of 1% and permeability 

of 16 md.

The average longitudinal wave velocity with natural moisture for 

the Proterozoic metasediments is 5.67 kmps, and that for the Archean 

rocks is 3.99 kmps. The idea that velocity of rocks of the same composition 

increases with depth is .not confirmed. Maximum values are found in the 

upper part of the section.

Magnetic susceptibility of the basaltic volcanics lies within a 

narrow range regardless of extent of metamorphism. Maximum values of 

this parameter are found for meta-trachybasalt schists and serpentinized 

peridotites. Minimum values are characteristic of dolomites and quartzites.
Natural remanent magnetization in the Archean rocks is in general 

lower than in the Proterozoic rocks. Maximum values were recorded in 

serpentinized peridotites of the Pechenga Complex.

The ratio of natural remanent magnetization to induced (Q) ranges 

from 0.1 to 29 and correlates with the composition of the magnetic 

minerals.

Drill hole SG-3 is divided into three zones on a basis of magnetic 

characteristics. The depth interval 0-4586 m is a zone of sulfide 

mineralization, and the rocks are weakly magnetic except for the ultramafics. The 4586-5642 m depth interval corresponds with a zone of oxide 

mineralization and is characterized by higher magnetic susceptibility. 

The 5642-10,500 m depth interval is a zone of weakly magnetic rocks; 

concentrations of pyrrhotite and magnetite are small.

Radioactivity was measured both in the drill hole and on samples. 

Uranium and thorium content of rocks was determined in the laboratory. 

Data were also obtained on the average life time of thermal neutrons.

The geothermal gradient increases with depth from 1-1.1°C/100 m in 

the upper part of the Pechenga complex to 1.7-2°C/100 m in the lower part 

at a depth of 6000-7000 m.

The following physical properties were measured on core samples; 

static Young's modulus, static Poisson's ratio, compressive strength, 

tensile strength, hardness, plasticity, and abrasivity.

An abrupt decrease in longitudinal and transverse wave velocities 

and in rock density is observed at a depth of 4500 m. This coincides 

with the boundary between the greenschist and epidote-amphibolite metamorphic facies. The deep seismic interfaces are caused by secondary 

transformations leading to a change in physical properties rather than by 

lithologic variability of the rocks.

Various stress fields are recognized in the section. These suggest 

that there is a clearly expressed horizontal layering in the crust, related not to extensive horizontal displacements but to changes in local 

conditions and mechanisms of deformation of the various deep horizons.

Drilling. A turbo drill was used in the project. Calculations 

indicate a significant advantage of turbo drilling over rotary drilling 

at depths greater than 10 km. Rates of 100-200 rotations per minute 

appear optimum. Steel is used for the upper 1.5-2 km of the drill string; 

then aluminum.

Actual drilling time was 21.7 percent of total time at 0-2000 m, 

whereas it was only 3.1 percent at 10,000-11,500 m. Drilling rate ranged 

from 1.3 to 2.5 in/hour. A total of 3700.1 m of core was recovered.
Foreword

The Communist Party of the Soviet Union and the Soviet Government at all 

stages of development of the state have given particular attention to 

strengthening the mineral resource base of the country and to improving 

exploration methods. For example, the economic plan for 1981-85 and on to 

1990 confirms the importance of accelerated geological study of the country. 

This study naturally is affected by fundamental understandings of systematic 

distributions of mineral resources in the deep subsurface, by new scientific 

ideas, and by their implementation.

The present book addresses one of the most important problems of modern 

Earth Science - a study program of the deep subsurface. Spudding in the Kola 

Superdeep well marked the beginning of a new stage in the study of the 

precambrian continental crust. The well is located in the northeast part of 

the Baltic shield in an area of junction of ore-bearing Precambrian structures 

typical of the basement of ancient platforms. The well is now at a depth of 

12,000 m. It has passed through the entire Proterozoic section and a 

considerable part of the Archean. Drilling continues. The present work 

presents briefly the main results of studies to a depth of 11,600 m in three 

sections: geology, geophysics, and drilling.

The first part of the book examines the geology of the well site; core 

and the wall rock of the drill hole are described in detail. Then data are 

given on the petrography and geochemistry of the Precambrian complex, 

metamorphic zones, vertical ore zonality, faults, gases, organic matter, 

subsurface waters, and finally the evolution of the continental crust for 

about 3 billion years.

The second part treats geophysical studies of the Kola well: physical 

properties along the section and the nature of geophysical interfaces. 

Techniques for study of rock properties were developed.

The third part deals with the drilling process to a depth of 11,600 m. 

The scientific-methodological basis for the drilling is presented, and the 

drilling equipment is described. The technical-economic results of the 

drilling are interpreted. The main tendencies and variations in the drilling 

processes with depth are analyzed, as are means for improving the technology 

for further deepening of this unique well.
The importance of mineral resources in the modern world increases 

constantly. Oil, gas and atomic raw materials are required more and more as a 

source of energy. The use of aluminum and titanium, light metals, 

particularly molybdenum, and also manganese, chromium, and nickel are 

increasing. Agriculture requires phosphates and potassium minerals. 

Electronics and space technology cannot develop without using rare metals. 

Economic potential depends ever more on mineral resources, and these 

requirements continue to grow.

Exploration for new mineral resources has turned to the shelves of 

continents beneath the seas and the floor of the ocean. Depth of exploration 

on the continents has increased (fig. I.I). Oil and gas are produced from 

depths of 5 to 6 km. Some gold mines are at depths of more than 3 km. Even 

iron ore is worked at a depth of 1 km at Krivoy Rog, and ore reserves are 

extended to 2.5 km depth. Most new deposits now being found have no surface 

expression.

Study of the deep subsurface of the USSR can be divided into three 

stages. The first was during the Sixties when plans were made to drill to 10 

to 15 km. The second was during the Seventies with experimental drilling 

in the Kola and Saatli superdeep wells. The third stage, beginning in 1981, 

is directed toward coordinated study of the crust and upper mantle of the 

entire country.

The objectives are the study of:

a) Sedimentary cover of deep depressions on eratons

b) Sedimentary section of geosynclines

c) Composition and structure of the lower part of the granitic layer, 

nature -v

£»of the Konrad discontinuity, and composition of the basaltic layer

d) Nature of the M-discontinuity, composition of the upper layers of 

of the upper mantle

e) Processes of differentiation in the crust

f) Magma chambers

g) Solutions and gases in the crust

h) Geothermal regime of the crust

1960-69. A group was organized that addressed "study of the subsurface 

and superdeep drilling." It coordinated about 200 scientific and industrial 

agencies, 4 academicians and 15 corresponding members of the Academy of 

Sciences, USSR; 5 academicians and 6 corresponding members of Academies of the 

republics; 70 doctors; and 65 "candidates [candidate is commonly equated with 

Ph.D.]. More than 80 conferences and 75 inquiry sessions were held. The Kola 

and Saatli sites were selected during this time.
Oceanic 

crust

Continental crust

Shelf zone Shield Platform Zone of platform downwarps

tuoCO

oD

Challengei

Kola 

SG-3

< £ 8 «' & 

< w rjoq: p

V V V V

V V V V V

V V V V

n n n n

n n n

n n n n

n n n

n n ' n n

n n n

n n n n

n n n

n n n n

n n n

n n n n

4- 4- 4. 4. + 4- 4- 20-30 KM 4- 4- 4-

v v- v v v

V V V- V v ^ *V V V" V" V"

v v v" v v >

 II- v ^25-50 KM v v ^ v 

n n n n n n n n n n n n

nnnnn-nnnnnnn 

nnnnnnnnnnnn

nnnnnnnnnnnn

J3 O Q D O a n n n - ^ n

V V V V

V VV

n n n n n n n

n n n n n n r

Figure I.I. Schematic section of crust from deep'drilling data.

Deep exploration drilling: I - in the shelf zone, II - for solid mineral 

resources, III - oil and gas wells.

1 - Hydrosphere; 2 - oceanic basalts; 3 - Phanerozoic sedimentary and 

sedimentary-volcanic rocks (age of 500 m.y.); 4 - Precambrian crystalline 

rocks of "granite" layer (age of 1,000-3,000 m.y. and more); 5 - rocks of 

continental "basaltic" layer; 6 - rocks of the mantle; 7 - high-velocity 

layer - Conrad discontinuity (vp = 6.6-6.8 kmps); 8 - M-discontinuity 

(v = 8.0 kmps).
1970-80. The program for the Seventies included development of a model of 

the crust and mantle, new methods of predicting mineral deposits, compilation 

of resource assessment maps, and planning for exploration in favorable regions 

of the country. The program for 1976-80 included 198 projects directed toward 

solution of applied problems related to fundamental theoretical analysis of 

the deep subsurface.

The lead agency is the Ministry of Geology, and more than 150 scientific 

and industrial organizations are involved.

Drilling of Kola SG-3 (fig. 1.2) was begun in May 1970. The purposes 

were:

1) Study of the deep subsurface of the nickeliferous Pechenga complex and 

Archean crystalline substrate of the Baltic shield.

2) Clarification of the geologic nature of seismic interfaces in the 

continental crust, and gaining new data on the thermal regime and on deep 

aqueous solutions and gases.

3) Obtaining information on the composition and physical properties of 

rocks, and study of the boundary between the granitic and basaltic layers of 

the crust.

4) Improvement and creation of new deep-drilling and geophysical-logging 

techniques.

By 1980 geophysical surveys had been completed in several of the regions; 

18,000 km of deep-seismic-sounding had been run. The relief of the Mdiscontinuity and the pre-Riphean surface had been mapped in East Siberia. 

New information was obtained on the upper mantle for the East European and 

Siberian cratons and the platforms and folcbelts that surround them. Velocity 

sections to 400 km were compiled.

Kola Super deep reached a depth of 10.7 km in 1980.

The composition and properties of the rocks were found to change 

systematically with depth. Vertical zonality in the metamorphic rocks was 

found to be different from the theoretical model.

Geothermal gradient was found to be steeper than, had been anticipated. 

The role of mantle and radiogenic sources in deep heat flow was determined.

The vertical geochemical section of the crust to a depth of 11.6 km 

disclosed a systematic variation with depth in the silicity and alkalinity of 

the rocks as well as in the behavior of metallic, .rare, and radioactive 

elements.
Figure I. 2. Kola superdeep, general view,
Commercial-grade copper-nickel ore was found in the 1665-1830 m interval, 

in the 6,500-9,500 m depth interval is a zone of copper-lead-nickel 

mineralization.

Unexpected was the occurrence at great depth of very porous, fractured 

rocks saturated by water. High permeabilities were also found. These 

disclosures are important for toxic waste disposal.

Kola superdeep did not confirm the geophysical basaltic layer at 

7,000-7,500 m depth; rather, dense Archean gneisses were present on through 

this level. This calls for a new look at the geophysics.

Yet another superdeep well, Saatli, was begun in 1977 in the Kura 

depression of Azerbaydzhan; it is on a long-known gravity high. The 

supposition was that this anomaly was due to a local uplift on the top of the 

basaltic layer. The hole passed through unconsolidated Cenozoic and upper 

Mesozoic sediments and then into a thick volcanic section apparently of 

Cretaceous age. These volcanic rocks are clearly the source of the gravity 

maximum.

Drilling rigs in world practice are rated for a lift capacity of 6-8 MN 

and a pump pressure of 50 mpa (mega-pascTaIs). Depth, however, does not 

exceed 9,100-9,600 m. Greater depths do not seem possible. The Soviet rigs 

with less lift capacity (5 MN) and injection pressure (40 mpa) are capable of 

depths greater than 10 km.

New drilling equipment was designed by Uralmashzavod (figs. 1.3, 1.4). .
Figure 1.3. Lowering of. drill string into well.
Figure 1.4. Core recovery.
1981-85. A new stage in the study of the deep subsurface began in the 

Eleventh Five Year Plan. A net of interrelated geophysical activities is 

to be set up:

Superdeep 

research 

drill holes

Deep

drill holes

Geophysical

research

profiles

Predictive 

polygons

Space-craft 

studies

Research net of the first class

Seisiaic 

profiles at 

1:500,000 

and greater

Aero-surveys at 

1:500,000 and 

greater

f \

Net of the second class

\/

Geological and geophysical maps and cross 

sections of the crust

Deep and superdeep-drilling will be expanded. Drilling of the Kola and 

Saatli holes will continue. The Tyumen, Anastas'yev-Troitsk, and Ural 

superdeep (12-15 km) holes will be-."begun. Drilling will also begin on six 

deep holes: Three (Dnieper-Donets, North Caspian,' Timan-Pechora) in oil 

patches and three (Muruntan, Noril'sk, and Krivorozh) in mining regions.
Kola Superdeep will reach 13,400 m during the Eleventh Five Year Plan and 

will intersect another geophysical interface , which may turn out to be the 

granite-basalt boundary. Saatli will be deepened to 11,000 m.

Drilling of the Tyumen superdeep hole will give information on the oil-gas 

potential of the Jurassic and pre-Jurassic section of the north of West 

Siberia. The Ural superdeep will yield information on a very large 

ore-bearing foldbelt.

At the time the Soviets were planning these operations, the Americans 

proposed an ocean drilling program. This program became international, and 

Soviet scientists participated. Thus, there are two programs: The Soviet on 

the continents and the international in the oceans, supplementing one another.

10
General Geology

GEOLOGY OF THE NORTHEAST PART OF THE BALTIC SHIELD

2 The Baltic Shield, 1,140,000 km , is the largest area of exposed

crystalline basement of the East-European Platform. The Kola Peninsula 

occupies the northeast part of the Baltic Shield.

Geology of the Kola Peninsula

The Kola Peninsula is composed mainly of Precambrian crystalline rocks 

(Fig. I, 6) which extend into Finland, Sweden, and Norway. These rocks are

Archaean gneisses with metamorphosed sodic-calqic oranitoids and Proterozoic metamorphosed sediments and volcanlcs. The Archean

rocks have been dated as no less than 2700 m.y. and possibly as much as 3600

m.y. Mineral resources include iron, titanium, copper, nickel, rare-earth 

metals, pegmatites, apatite, nepheline, and others.

Subsurface Geology of the Kola Peninsula

The main source of data on the subsurface is from deep seismic sounding 

and seismic reflection studies. The average depth of the Mohorovicic 

discontinuity on the Kola Peninsula is 37 km with a range of 28 to 40 km (Fig. 

I, 7). The most important boundaries above the M-discontinuity are the Konrad 

discontinuity, at the top of the granulite-basite or basalt layer, and another 

at the top of the diorite layer.

Geology of the area of corehole SD-3

The area of the corehole is composed of ancient crystalline rocks, 

metamorphosed to various degrees, characteristic of Precambrian of the Baltic 

Shield (see Fig. I, 8. in pocket). Of continuing interest to geologists in 

this area are copper-nickel deposits associated with Proterozoic ultrabasic 

intrusions. The following Precambrian complexes are recognized in this area: 

Archean, forming the folded basement and in tectonic blocks; and Proterozoic, 

composed of T£ne±arnorpfrbsed sedimentary and volcanic rocks.

Archean

In the area of corehole SD-3 the Archean Kola Series is divided into two 

sequences: biotite-plagioclase and biotite-amphibole-plagioclase gneiss and 

amphibolite at the base, and biotite-plagioclase and muscovite-biotiteplagioclase gneiss with high-alumina minerals (staurolite, andalusite,

li
sillimanite, kyanite, garnet), and rarely interbeds of amphibolite, above. 

The lower sequence locally contains interbeds of magnetite-garnet-quartz 

feldspar schist and ferruginous quartzite, which are generally no more than 

20- 30 m thick. The gneisses are irregularly granitized locally with 

formation of migmatite. The rocks of the Kola Series are metamorphosed mainly 

to the amphibolite facies.

Proterozoic

The Proterozoic section consists of sedimentary and volcanic rocks of the 

Pechenga and Varzug complexes and the Tundrov Series adjacent on the south. 

The Proterozoic rocks directly overlie folded Archean gneisses of the basement 

in a transgressive sequence with conglomerate at the base.

Results of deep geophysical studies in the area of corehole SD-3.

The first studies in the Soviet Union on the crust in shield areas were 

deep seismic sounding studies in the Kola Peninsula in 1960-1963 (Fig. I/ 

9). Crustal thickness in the vicinity of the corehole was shown to be about 

40 km. The early seismic work showed a total thickness of 7-8 km for the 

sedimentary-volcanic rocks, and essentially no granitic layer. Reflection 

seismology was later used to determine the structure to depths of 10-15 km. A 

gravity survey was made in 1967-1969, which confirmed the conclusions of the 

seismic work.

The Kola superdeep corehole should answer many questions about the Baltic 

Shield and the crust in general, such as:

1) Stratigraphic subdivision of the Proterozoic and especially the 

Archean: age, thickness, structure.

2) Composition of the sedimentary-volcanic "superstructure" above the 

Archean basement.

3) Test the presence of deep ore horizons.

4) Sequence of metamorphic processes in tjie Precambrian.

5) Vertical zonation of hydrothermal mineralization.

6) Decrease in rock fracture with depth.

7) Gas emanations, and depth of water-bearing horizon, related to the 

preceding question.

8) Paleotemperatures and the present thermal gradient.

9) Lithostatic pressures with depth.

10) Nature of geophysical boundaries.

12
GEOLOGIC SECTION OF THE ODRSBDLE

The results of study of the core have been compiled in geologic and 

geophysical columnar sections (Fig. I, 10, 11, 12, 13). The hole penetrated 

_the Pechenga sedimentary-volcanic complex and at 4700 m entered Archean 

gneisses, and'at 7-8 km depth encountered the high-velocity layer, granulitebasite (Fig. I, 14).

Stratigraphic subdivision of the section

Tables I, 1, 2 present specific depths at which contacts were picked for 

the individual suites of the Pechenga Complex (Lower Proterozoic) and Kola 

Series (Archean).
fD

Oi

\v

r

\

_i

lilit^S

; x ; vYi\\^^^x*\\^

1 V rV\rA^\\V v\ iM i\v v.i.v.v ^J
Fig. i t 6. Geologic map of the Kola Peninsula. Paleozoic: 1) Upper Devonian 

and Lower Carboniferous, sedimentary-volcanic complex of the Kontozer 

structure. Upper Proterozoic; 2) formations of the Hyperboreal Series of the 

Rybach'ev Peninsula: conglomerate, sandstone, shale; Srednii Peninsula, 

Kil'dina and Terskaya Islands: quartzite, sandstone, variegated shale/ 

dolomite. Lower Proterozoic: 3) Pechanga, Imandra-Varzug, and Kuolayarvin 

complexes: basic, medium, and ultrabasic lavas, tuffs, minor phyllite, 

silts tone, sandstone, dolomite, and conglomerate, metamorphosed mainly to 

greenschist facies. Lower Proterozoic-Upper Archean: 4) Keiva Series: 

aluminous, carbonaceous, micaceous, and other schists, quartzites, and 

sandstones, metamorphosed mainly to epidote-amphibolite facies; 5) Tundrov 

Series: araphibolitic, micaceous, aluminous schists and gneisses, amphibolite, 

ferruginous quartzites, metamorphosed mainly to epidote-amphibolite facies. 

Lower Archean, Kola Series: 6) biotite-plagioclase, biotite-amphiboleplagioclase, two-mica gneisses biotite-plagioclase gneiss with HAM 

(high-aluminum minerals), araphibolite; mainly amphibolite facies; 7) 

biotite-plagioclase gneiss with HAM, araphibolite, pyroxene-amphiboliteplagioclase gneiss and schist, ferruginous quartzite, mainly amphibolite 

facies; 8) granulite complex: cordierite-garnet-biotite-plagioclase gneiss 

pyroxene-araphibole-plagioclase gneiss and schist, amphibolite and migmatite, 

charnockite, enderbite, mainly in granulite facies. Intrusive and 

ultrametamorphic complexes: Middle Paleozoic (Upper Devonian): 9) silicic 

nepheline syenite complex; Lower Paleozoic: 10) basic, ultrabasic and 

alkaline rocks; Upper Proterozoic; 11) gabbro, diabase, granophyre; Lower 

Proterozoic; 12) granite, granodiorite; 13) alkaline granite syenite; 14)

-\ ' 

gjabbro, gabbronorite, pyroxjenite, peridotite, olivinite; Upper Archean; 15) 

granite, granite-migmatite; 16) gabbro-anorthosite, metagabbro-norite; Lower 

Archean; 17) granite, granite migmatite; 18) granodiorite, granite-gneiss, 

plagiogranite; 19) major faults (I. Karpinsk; II. Keiva-Uragub; III, 

Pechenga-Varzug; IV, Lapland-Kolvits); 20) zone of maximum Caledonian 

activity; 21) explosion vents; 22) Kola superdeep corehole 

Key: 1) Barents Sea 

2) Kandalak Bay

is"
Fig. I, 7. Subsurface geology of the Kola Peninsula. 1) contours on the Mdiscontinuity (in km)' 2) isolines of increase in force of gravity 

field; 3) isoclines of relative decrease in gravity force field;

^

4) major faults; 5) simatic crust; 6) sialic crust. 

Key: © Barents Sea

2) White Sea . .

N.
-av

H

0.

<1$Q

2D

W

v cr-3 NI

33 , . 

;07<M W W 50 h 0 50 W*»

* S.i* « 5.9-5. * ') M S.?-$.3 ' »>-».}, y ^ ;/ - . . TT^T'^y^-Ja l * g/TTT"^*'^ ' : " ' > .. ' ' ' ' ^ M ' * -A^r S t ', t .< ,*: 7- . ^-ria-^/U-J-^- 1. "-u J- * * * * * ' 1-^-- 

v Av ^ v v >A v -j , , ^v v//' -i_i__ ^J v v '\ v v v ...,..*... . . r-r

L V V ^ »,;. '-?( ^ ^^^" ^ " " - " « " "

Fig. I, 9.--Seismic section of the crust along the profile Lovno-PechengaBarents Sea. 1) Average position of reference (a) and other (b) 

seismic boundaries; 2) velocity (upper, average; lower, boundary; 

km/sec); 3) Phanerozoic sedimentary rocks; 4) same-, Riphean; 5) 

lower part of the "basaltic" layer; 6) schist and araphibolite; 7) 

gneiss complex; 8) gneiss, granite gneiss, granite; 10) basic and 

ultrabasic intrusions; 11) middle non-uniform part of the basaltic 

layer; 12) Pechenga sedimentary-volcanic series; 13) upper mantle; 

14) fault.

17
// n p o P 0 O U C H a j^

u

T o n o n OHOQCHOH

rii :

o m e p 

\ I V \ A V\ VT

ri 

" 

r) 

\ \ >

oc

i i, i_

1,0 f*

jNra

A'til

U4 i ^

Lll o R

^ * L'J

0

Apnfi'icnOH t pv tin a

KQ/lbCHQH C f P U H M-

'V 'i,

1*1- « .1"

\ \ \ \

// n p o in e p p__j

i'f. ~~TI e~ * e n e 

o 

c

u c H 

n u u

y o c fit o p u H c H a a

.1,. i. i. i

i r-r

^i2_J Q?p±

l^tyfapti

1 I uiJOHC _____J. .- 

Hep*neflvoC'uopuHc]iai&

H u 

26

r \ 

»-*J

D

?/ n r*^ / 

M 

L°

j i i i

X~\ 'k ^ ^ \ \ \ 
Fig. I, 10. Columnar section of the Kola Superdeep corehole (SD-3). Pechenga 

complex: 1) augite diabase., 2) basic tuff; 3) pytoxenitic and picritic 

porphyrite; 4) rhythmically bedded phyllite, siltstone, sandstone, tuffite, 

and tuff; 5) rhythmically bedded sandstone with minor siltstone and phyllite; 

6) actinolitized diabase; 7} amphibole and biotite-chlorite schist with 

ultrabasic tuff; 8) dolomite; 9) arkosic sandstone; 10) sericite schist 

(weathering rind); 11) raeta- :diabase, raeta-andesite/ meta-albitophyre, with 

banded lava, tuff, and greenschist; 12) dolomite, marble, and polymictic 

sandstone; 13) diabasrc porphyrite, biotite-amphibole-plagioclase schist in 

andesite-basalt; 14) polymictic -conglomerate, gravelite, sandstone; 15-18) 

intrusives; 15) ancesitic porphyrite; 16) gabbro-diabase; 17) essexitic 

gabbro; 18) wehrlite; 19) sulfide copper-nickel ore. Kola series: 20) 

biotite-plagioclase gneiss, schist with HAM (high alumina minerals); 21) 

biotite-plagioclase and biotite-amphibole-plagioclase gneiss, schist; 22) 

amphibolite; 23) talc-biotite-actinolite schist (in ultrabasic rocks); 24-26) 

intrusives: 24) plagiomicrocline granite, pegmatite; 25) metagabbro; 26) 

plagiogranite and dark migmatite; 27-29) ore; 27) magnetite; 28) 

titano-magnetite; 29) cataclastic and mylonitized zones. Sequences: I) . 

muscovite-biotite- plagioclase gneiss with HAM (andalusite, staurolite, 

sillimanite, garnet); II) biotite-plagioclase and 

biotite-amphibole-plagioclase gneiss and amphibolite; III) 

muscovite-biotite-plagioclase gneiss with HAM (silliminate, garnet); IV) 

biotite-plagioclase and bioti'te-amphibole-plagioclase gneiss and amphibolite; 

V) muscovite-biotite-plagioclase gneiss with HAM (kyanite, sillimanite, 

garnet); VI) biotite-plagioclase gneiss and amphibolite 

Key: 1) Strati graphic subdivision 17) Zhdanov

2) Group 18) Matertin

3) Complex 19) Luostarin

4) Series 20) Lower Luostarin

5) Subseries , 21) Upper Luostarin

6) Formation . ' - 22) Televin

7) Depth, m 23) Mayarvin

8) Lithologic column 24) Kuvernerinuok

9) Attitude of rock - .. 25) Pirttiyarvin "

10) Sequence 26) Luchlompol

11) Proterozoic 27) Zapolyarnin

12) Pechenga 28) Archean Group

13) Nickel 29) Kola Series

14) Lower Nickel 30) Archean

15) Upper Nickel ( 31) Kola
Fig. I, 11 Parts of Kola coreho-le SD-3 in the intervals 2730-2830 m (a) and 

4770-4900 m (b).

1) Gabbro-diabase; 2) saadscone; 3) phyllite; 4) diabase, 

actinolitized; 5) andesitic porphyry, 6) dolomite; 7) dolomitic 

sandstone; 8) sericitic schist (weathered rind); 9) schistose 

diabase.

Key: 1) Depth, M

2) Lithologic column -" -- . ' 

3) Amount of core, %

4) Calliper

20
Fig. I, 12. Parts of the Kola corehole SD-3 in the intervals 10,550-10,640 m 

(a) and 11,360-11,460 m (b). 1-3) biotite-plagioclase gneiss; 1) 

with HAM, 2) with kyanite, sillimanice, garnet, 3) with garnet, 

sillimanite; 4) biotite-amphibole-plagioclase gneis's; 5) 

atnphibolite; 6) talc-biotite-actinolite-schist (in ultrabasic 

rocks); 7) granite; 8) pegmatite.

Key:(T) Depth, M

(2) Lithologic column 

("$} Amount of core, % 

,(4) Calliper

BK - Laterolog

FK - Gamma log

(4) AK - Acoustic log

/055tf-.~-^~-rHQJ\QH*a 3^ 4*

*XW + jr I

125 25 J7J>i»tO /5yc3».«[/25 1S5 '205

§ = jBi

nxo

mso_ 

TWO

iUTOjioeuu.

HQJIQHHQ

V V V

/ t y

]

ifS =X 3 * 

^ *

n

KCdSpHCMeTpUfi 

30 «^CM

r/f 

/0 /J ^<7 vw ra 125 !65

AK

205 MKC/f

^_ 

£"W. ?'

^1

^tf-

">£"

:^"
Fig. 1, 13
Fig- I,

Key:® 

©

13.--Geologic and geophysical section of Kola corehol^. SO-3.

1) Augite diabase with pyroxene and picrice pcrp li.vry interbeds;

2) tuff and tuffite of basic composition; 3) phyllif.^.. si It stone, 

with tuff interbeds: 4) rythmicaiiy bedded sandstone with lesser 

siltstone and phyllite; 5) actinolitized diabase; 6) dolomite, 

arkosic sandstone; 7) sericit schist; 8) metadiabase; 9) 

dolomite, polymictic sandstone; 10) aiabasic poryphyry and 

schist; 11) polymictic conglomerate, grav^Kfcfe; 12; biotiteplagioclase gneiss with HAM; 13) tr.ignva cized and grsnitized 

biotite-plagioclase gneiss; 14) magnetite-amphibolite schist; 15- 

18) intrusives: 15) andesitic porphyry, 16) wehrlite, 17) gabbrodiabase (dagger: granite), 18) fault. Sequences I, III, V, VII: 

muscovi te-biotite-plagioclasae gneiss with HAM ( andalusite* 

staurolite, sillimanite, garnet) with amphibolite bodies; 

sequences II, IV, VI: biotite-plagioclase gneiss, biotiteamphibole-pla'gioclase gneiss and amphibolite. 

Group

Series

Suite, sequence 

Lithologic column 

Archean 

Proterozoic 

Kola series 

Pechenga Complex 

Luostarin, Nickel

Gamma log

II) Resistivity log

Caliper r?J' log

Acoustical log

Vertical seismic profile (?)

23
^ v.

<a

nj| a^

a p

ll« c

* M£ *. f

S£

i <:

^S Q

<J Ica vj

a;

^ Cx

o

^

i

I

 ^ *a 

^* o

Q

ys

0

2-

^

^

^

c 

51

N^

f4

^ ^

Q S

2.5 "^ 5

^

4j

^1

0

u

w

nso

MOO

J650

4080

4100

^660

7000

moo

 J V

V

<S V *

\f V

V V

 S V 

V V \S

v v v

_ _ _ .

_~"_~_~

~-_~_~-

_

_r_r_~

- -^

^ ^

 -

 ~

-~ 

-^ -^ _ ~

-^ -^»

-*""-.""

-. ^.

"-."",.;

 x

V,

\

\

\

\

^\

^ ^".,

\\ 'Xx

\\ \

\\\

Q

c

?

<

^> ^

^

a.

i

'cs 5

§ ^

M

i

<^

^

^

QC

Q

C

u

4

^

1

*

<^

^*

"

SQ*

M

CM <x

?,

a a. 6°

Q

^

^~

%^

x

 s.

W59

2305

56*2

sin

S82J

68^2

\

fMOO\

V V V

V V

-/ V V

V -J 

V V V

. '<

V V V 

 / V

V V V

V V

V v

\/ V V

V V

V V

V V V 

V V 

V V V

V V

V V V

Ir- 3-1

-£-~-

~v~*_~

 - - 

 

 . 

 

_ _ _

>>;

-~-~=i

Fig. l r 14. Comparison of the section at corehole SD-3 as projected from

seismic studies (a) and from the core (b). 1) effusive rocks of mainly basic

t 

composition; 2) sedimentary rocks; 3) gneiss, granite gneiss, and amphibolite;

4) granulitic basalt; 5) gneiss, and amphibolite in a high metamorphic facies;

6) fault.

Key: 1) Sedimentary-volcanic rocks of the

Pechenga Complex (Lower Proterozoic)

2) Luostarin Series

3) Nickel Series

4) Kola Series (Archean)

5) Granulite-basite sequence

24
See next page for translation.

CTPATHPPAOMMECKOE PACMJ1EHEHME nEHEHPCKOro KOM H.- 

(HHXHMfl HPOTEPOSOH) no PA3P£3>' CK8 CT-3

T A 6 .1 I! U A ! i

/

'-rp.ii!

_

^

o

r

-£.

 £

/2.^*

^^^ r

\

=

H>

O

^

7

Caitia

MaiepTiiHCK3H (m/)

/KJ3HOB- ^

CK3H (g(f)

^

33no.isp^

HHHCK3H i-|0

' (-P) Xl

.lVM.10.Mno.ibCKaH : ^

(/*) ^/

iliipTTnap-!

BllHCK3fl J^

(pr) ^s- r\

PMHHOKCK3H i

MaflpenH- ]

CK3H (ma).', r

Te.ieBHH-"^

CK3JJ (//X1 )/"

llHtf pna.i3

6ypeHti<i, M

9-1059

1059-2805

/

q _ "I'

2805 4673

IK

4673-4884 '

il-1

4884 5642

\$"

5642 5717,

/* (7-1

5717 6823

I ,q6823 6842

2o # '

 7

/ y f * «,

 ~3

KOii/rt.T.rT,.. «

./_liia6a3u uiapOBbi.x 11 MacciiBHu.x .iad 1G50

C nOaMHHCHHUMII TlpOCvlOSMll TV^OH, ;

nHKpiiTOBbi.x M nnpOKceHoau.x ;icp4)i! 1

^DIITOB

TOHKOpllTMIIMHbJe a^CBpO^HTW, (pll.1.1!!-

TbJ C npOC.IOHMII Ty(|>OB H neCM3H!!K03.

O.iHro.MiiKTOBhie M no.iHMHKTOBbie necMaHIIKI! C npOC-IOHMK XOHiMOMCpaTOn,

.011^111X00 It 2.leBpO^HTOB

AKTUHO.1HTH3HpOBaHHhie Jl!a6a3U UJ3-

pOBblX 11 MaCCHBHUX .138 C nOJHMHeHHbiMii npoc.iOHMii Ty4>oreHHhi.\ nopoa

**Zlo.1O.MHThl, J0.1O.MI!TOBble nCCMaHIIKII,

apxo3OBt>ie necMaHiiKit c npoc.iOHMii

a.ieBpo.niTOB

/MeTaana6a3bi, MeiaaHaesiiThi, c.iaH^u

no jnaCasaM M 3Hae3i!TaM, B T. M. no-

' Tpe.Mo.iiiT-KapfioHaTHbie c.iaHUw. vpaMOpII3OB3HHbie II3BeCTHflKH, KB3pU)ITC-

^A.v(|)i!6o.i-n*iariioK.Ta30Bbje H 61101111-

a.M(|)n6o.i-n.ianiOK.Ta3OBue 'c.iaHuw (no 

<sj.na6a3a.M)

^MeTanecsaHHKii n MeTarpaBe.uiTbi

! / -i G

1868

LM I

758

75

1106

19

25
Table I, 1. Stratigraphic subdivision of the Pechenga Complex (Lower 

Proterozoic) at corehole SD-3. 

Key: 1) Series

2) Formation

3) Interval

4) Characteristics of the rock 

5} Vertical Thickness, ra

6) Matertin (mt)

7) Diabase, spheroidal and massive lava with minor interbeds of tuff, 

picrite, and pyroxene porphyries,

8) Zhanov (gd)

9) Finely rhythmic siltstone, phyllite, with interbeds of tuff and

sandstone. Oligornictic and polymictic sandstone with interbeds of 

conglomerate, phyllite, and siltstone.

10) Zapolyarnin (zp)

11) Actinolitized diabase, spheroidal and massive lava with minor 

interbeds of tuffaceous rocks

12) Luchulompol' (Iz)

13) Dolomite, dolomitic sandstone, arkosic sandstone with interbeds of 

siltstone

14) Pirttiyarvin (pr)

15) Metadiabase, meta-andesite, schist in diabase and andesite, including 

banded lava

16) Kuverneriniok (kw) ,

17) Tremolite-carbonate schist, limestone marble, quartzose sandstone

18) Mayarvin (ma)

19) Amphibole-plagioclase and biotite-amphibole-plagioclase schist (in 

diabase)

20) Televin (tlw)

21) Metasandstone and metagravelite

22) Nickel

23) Luostarin

26
T A 5 .1 11 U A i .'

CXEMA CTPATHrpA*HHcCKOro PACMwlEHEHHfl KOjTbCKOK CEPHH 

<APXEH) HO PA3PE3V CKB. Cf-3

f

>« To.imn

I

II

.

HI

IV

V

VI

VII

MVpemi*. M

6842 7622

/

 3

6842 7271

(a

7271-7622

7

7622-9456

*

7622-8465

Q

*

8465-9456

(0

9456 9573fl

R

9573 10 144

10144 10301N*

10601 1I4I6

11416 11662 16"

XapaKtepiicTiiKa TQ.IUI

MycKO8iiT-6uoTiiT-n.TariiOK.ia30Bue rHeucu c

BFM (3Haa.iy3itT, CTaspo-iiiT, cn.i.iii.MaHiiT. rpaH3T)

BepxHHH nacTb TO.ILUII MycKOBiiT-6iiOTitT-n.iarnoK.Ta303b(e rneucbi c 3PM

Hl!>KHHfl MaCTb TO.TLUU MyCKOBIlT-6HOTllT-n^3-

riioK.Ta3oabie rneucbi c BfM u re.ia.Mii ast4)ii6o-

.1IITOB

BiiOTur-n.iariioK.ia308ue u unoTiiT-aM(|)it6o.i-n.iarilOK.1330Bbie rHCl'lCbl 1< a .\ICpn6u.1llTb4

BepXHflH vacTb TO.ILUII 6iioTitT-n.iariiOK.Ta30-

swe rHeficbi 11 3Mc|;ii6o.iiiTbJ npeiiMyuiecTBeHHo c

KVMMHHrTOHUTOM

HlI>KHHfl M3CTb TO.TLUJI 6llOTIIT-n.ianiOK.Ta3Oawe. 6iiOTi[T-a.M<|)ii6o.T-n.TaniOK«i3308bie rHeficw u

a%it|)ii6o.iiiTbj

\\ycK08tiT-6iiOTiiT-n.iarnoK.ia3OBbie rweiicu c

Bf"M (ClI.l.lllMaHlIT. rp3H3T)

^

5llOTllT ^.^a^llOK.^a3O3ble r»eficu u a\:4>ii6o.inTbl

.\\\CKOBiiT-6noTiiT-n.TanicK.ia3OBbJC rHeucu c

1 BPM (KiiaHiiT, ciu.iitMamiT, rpaHaT]

5noTiiT-n.TaniOK.Ta3OBbie rHei'icbi }H

5iioTiiT-n.TaruoK.ia30Bbie rHef<Cbi c BfM (rpa-.

H3T, CI(.T.T.ItM3HHT) 11 3 M(|)1|60.11IT08 C rpaH3TOM

BepTiiKJ.it>Ha«

MUUUHOCtb. M

780

430

350 

1830

840

990

120

570

460

820

250

27
Table I, 2. Stratigraphic subdivision of the Kola Series (Archean) at

corehole SD-3.

Key: 1) Sequence no.

2) Interval/ m

3) Characteristics of the sequence

4) Vertical thickness, m

5) Muscovite-biotite-plagioclase gneiss with HAM (andalusite, 

staurolite, sillimanite.^ garnet).

6) Upper part of sequence: muscovite-biotite-plagioclase gneiss with HAM

7) Lower part of sequence: muscovite-bioti te-plagioclase gneiss with HAM 

and amphibolite bodies

8) Biotite-plagioclase and biotite-amphibole-plagioclase gneiss and 

amphibolite

9) Upper part of sequence: biotite-plagioclase gneiss and amphibolite, 

principally with cummingtonite

10) Lower part of sequence: biotite-plagioclase, biotite-amphiboleplagioclase gneiss and amphibolite

11) Muscovite-biotite-plagioclase gneiss with HAM (sillimanite, garnet)

12) Biotite-plagioclase gneiss and amphibolite

13) Muscovite-biotite-plagioclase gneiss with HAM (kyanite, sillimanite, 

garnet)

14) Biotite-plagioclase gneiss

15) Biotite-plagioclase gneiss with HAM (garnet, sillimanite) and 

amphibolite with garnet

28
Rocks and Rock-Forming Minerals

Volcanic, sedimentary and intrusive rocks, metamorphosed to varying 

degrees, as well as, . ' / ./.\ultrametamorphic rocks, occur in the 

section penetrated by the SG-3 drillhole. The upper part of the section is 

represented by a Proterozoic metamorphosed sedimentary-volcanic complex and 

the lower part by an Archean polymetamorphic complex.

Metamorphic and Intrusive Rocks of the Pechenga Complex 

Basic volcanic rocks make up more than 70 percent of the Pechenga 

Complex, the remainder being composed of intermediate and ultramafic volcanics 

and tufogenic-sedimentary rocks. The latter includes tuffs, welded tuff 

breccias, conglomerates, gritstones, sandstones, siltstones, pelites, and 

carbonates. Cn the basis of mineral composition and paragenesis, the 

intensity of the regional metamorphism increases with depth, from prehnitepumpellyite to epidote-amphibolite with local appearances of amphibolite 

facies.

Volcanic Rocks

Diabasic volcanic rocks occur in the Matertin, Zapdyarnin, Mayarvin, 

Pirttiyarvin, and Zhdanov Formations.

Magnetic structures and minerals occur in the volcanic rocks in the 

upper part of the section, while a combination of primary magnetic features 

and neogenic metamorphic structures and minerals occur in the middle part, and 

neogenic metamorphic minerals, structures, and textures in the lower part of 

the section. The rocks are not uniformly metamorphosed, and the mineral 

composition is usually heterogeneous. Massive rock varieties yield to 

schistose varieties at depth.

Basalts are composed of pyroxene-augite and volcanic glass, with 

occasional laths of albitized plagioclase. Diabases are composed mainly of 

pyroxene-augite, salite, plagioclase, with rare hornblende and quartz.

The volcanic rocks in the section suggest, two types of volcanic 

activity: trachy-andesite basalts (Mayarvin and Pirttiyarvin Formations), and 

picritic basalts higher up in the section (zapolyarnin and Matertin 

Formations).

Sedimentary-Rocks

Tufogenic-sedimentary rocks include tuffs, tuff breccias, and tuffites 

(Matertin, Zhdanov, Zapolyarnin and Pirttiyarvin Formations). Phyllite and

29
phyllitic shales, siltstones, sandstones, sedimentary breccias, carbonates, 

gritstones, and conglomerates are present in the Zhdanov Formation. Ore 

minerals here include pyrite, pyrrhotite, sphene, and leucoxene. The 

Luchlompol Formation contains widely developed arkosic sandstone, siltstone, 

conglomerate, gritstone, and carbonate. The rocks of this formation are 

enriched in hematite and magnetite. The carbonates are enriched in 

tourmaline, rutile, anatase, and apatite. The Kuverneriniok Formation 

contains quartzites, meta-sandstones, siltstones and carbonates. Some rock 

varieties are enriched in allanite. The Televin Formation includes 

conglomerates and micaceous sandstones. Carbonaceous matter is found in 

phyllite and siltstones of the Zhdanov Formation, tuffogenic rocks in the 

mtertin Formation, and sedimentary rocks of the Luchlompol and Kuverneriniok 

Formations.

Intrusive Rocks

Intrusive rocks include ultrabasites, gabbro-diabases, and 

andesite-dacite porphyry. The ultrabasites are werhlites and serpentinites; 

associated minerals are pyrrhotite, pentlandite, chalcopyrite, pyrite, 

magnetite, ilmenite, apatite, garnet, and chromite. Sulfide copper-nickel 

mineralization is found. Gabbro-diabases occur in the depth interval 93.3 to 

2,754 m among rocks of the Matertin, zhadonv, and Mayarvin Formations. 

Accessory and ore minerals are sulfides, magnetite, ilmenite, apatite, and 

sphene. There is also titanium (0.7%), chromium (0.02%), and vanadium 

(0.03%). Andesite-dacite porphyry occurs in the depth interval 4,673 to 4,784 

m among rocks of the Luchlompol Formation.

Polymetamorphic Rocks of the Archean Complex

The Archean complex starts at a depth of 6842 m in the Kola Series, 

which is composed of gneisses with high-Al minerals, amphibolites, 

meta-ultramafites, granitized gieisses (piagio-granites, granites, pegmatites) 

and amphibolites. Small granite intrusions occur at 9,600 m.

Gneisses and Granitized Gneisses

Gneisses make up the larger part of the section penetrated. In the 

muscovite-biotite-plagioclase gneisses with high-Al minerals, the accessory 

minerals are apatite, magnetite, ilmenite, and zircon. The rock structure is 

lepidoheteroblastic, locally porphyroblastic. Biotite-plagioclse gneisses

30
with high-Al minerals have an insignificant admixture of Cr205, SrO, and 

BaO. Biotite is represented by three generations: Biotite from the granulite 

facies occurs at 10,222 m; biotite from the amphibolite facies occurs at all 

depths in the section in these rocks; and biotite from the epidote-amphibolite 

facies is also widely dispersed. Muscovite replaces biotite. Garnet occurs 

in two generations from the amphibolite facies and the epidote-amphibolite 

facies. Epidote is characteristic in biotite-plagioclase and granitized 

biotite-plagioclase gneisses, also forming two generations. Sphene also has 

two generations, the first being enriched in titanium.

Amphibolites

Three types of amphibolites are present in the drill-hole section. 

Hornblende amphibolite occurs along the entire section of the Archean. It is 

composed of hornblende with lesser amounts of plagioclase and biotite. 

Cummingtonite-hornblende-amphibolites are restricted mainly to 

biotite-plagioclase gneisses and alumina-amphibolites. The cummingtonite is 

replacing hornblende. The third types is an amphibolite transitional to 

hornblendite (ferruginous amphibolites). It is first noted at a depth of 

8,465 m and is composed primarily of hornblende and plagioclase. At depths 

greater than 10,000 m garnet is present. The structure of the amphibolites is 

grano-nematoblas tic.

Meta-ultramafites

The meta-ultramafites are ultrabasic rocks metamorphosed to actinolites 

and talc-actinolites. Actinolite is the most widespread and has an iron 

content of 22 to 23 percent (actinolite in talc-actinolite rocks has an even 

greater iron content). Actinolite is replaced by phlogopite, which is present 

in two varieties - iron-bearing (with a small admixture of titanium) and noniron-bearing. The rock structure is lepidoblastic.

Rock Alterations in the Polymetamorphic Complex

In the Archean metamorphic structure, six processes are distinguished in 

the drillhole: Metamorphism of the granulite facies; regional metamorphism in 

the amphibolite facies contemporaneous with folding; retrogressive regional 

metamorphism in the epidote-amphibolite facies; regional granitization under 

the epidote-amphibolite facies - the formation of palgiognanites and granites 

together with gneisses by metasomatic means; local manifestation of

31
diaphthoresis in the greenschist facias along fracture zones; local 

low-temperature metamorphism along zones of cataclasis.

The Temperature of Metamorphism

To estimate the temperature of rock metamorphism, equilibrium pairs of 

minerals were used, which include amphibole-plagiociase; amphibole-biotite; 

garnet-biotite; muscovite-biotite; and plagioclase-potassiura feldspar. The 

polymetamorphic Archean complex formed under a large range of temperatures. 

The temperature regime of metamorphism is: For the granulite facies, 1,000 to

I,200°C; for the amphibolite facies, 800 to 850°C (including regional 

metamorphism at 700-to 750°C); epidote-araphibole facies, 650 to 500°C 

(including granitization under the epidote-amphibole facies at 650 to 600°C).

Rock-Forming Minerals in the Subsurface Vertical Section

The age of the crust penetrated by the drillhole is 1.6 to 2.8+ b.y. The 

main rock types occurring in the Proterozoic section are metamorphosed 

magmatic rocks such as metabasalts (diabases and actinolite-diabases; 

apodiabasic-magnetite-amphibole-plagioclase schists; apodiabasic-amphiboleplagioclase schists), meta-andesites (apoandesitic magnetite-biotiteplagioclase schists), metapicrites, metagabbro, metawerhlite, and metasedimentary rocks (pelites, silts tones, sandstones, conglomerates, and 

carbonate rocks). The main rock types in the Archean are biotite-plagioclase 

gneisses, amphibolites, meta-ultramafites., plagiogranites, and granites. 

Biotite is found primarily in- the Archean complex, at depths of 6,842 to

II,662 m. Garnets.are found primarily in Archean gneisses. The composition 

and properties of the main types of rock-forming minerals of the metamorphic 

rocks were determined for their location in the drillhole's vertical section; 

this allows the possibility of estimating P-T conditions of the metamorphic 

rock at various stages of development.

32
XMMHHECKHH CC7CTA1

<?-f rvi/n cr AWX^^ ^\ to A if~<

H3 METABA3HTOB hEHEHFCKOro

PreVmiit-V, 

npcNiiT-nyMne

AnoAHa6a>oaai nopoaa 

pcHiiT-nyMilcjjiunroii

OKIICJM

<paun«

060. :»21>6 '

$L

060. 2305 . 8585

Ilopo.ia A»rirto-cajiiiT Oopoia 

<KocX

_ 060. woe

AKTUHOJIIT

. ssoa

riopoji

ofl. 19663

Poroaa* 

«X)M«HK«

tri. .19 663 

njartttKJai 

SiO,

TiO,

Al aO,

Fe,0s

TeO

MnO

MgO

CaO

NajO

KaO H,On. n. n.

47,70 

1.36

13.67 

2.01

12.01 

0.20 

7.00 

6.30 

1.66 

1.66 

0.22 

Me onp.

"5.22 

99.01

48.90

0,92

4.37

3,05

10,50

0.25

14,66

16.20

0.40

0,07

0.82 

He onp.

ibo.i'i

47.42 

0,83 

15,72 

3.23 

9,70 

0.17 

7.00 

9.50 

1,08 

0.47

He o6n.

He onp.

0.10

3.47

98,69

54,98

0,07

1,68

I.41

II.27

0,18

15,97

12,84

He o6n.

0.08

He odd. 

2,13 

He onp.

ibo.ei

64,11

0

21,99

He oCn.

3J3

9,86

0.10

He odx.

99.19

49,49

0,79

12,54

6.66 

8,91 

0.17 

6.62 

9.65 

2.73 

0.97

He o6n.

He onp. 

0.76 

1,16 

100,45

49.25

0,48

6,52

3.16

14.59

0,35

10,66

11.11

0,77

0,47

2.02 

He onp.

99,45

62,56

He o6H.

24.06

5.32 

8.69 

0.16

He onp.

He o6n.

100.77

n p M^K e^i H H e. ^AHa^iHTHKH^B. C. Ee-ioaa. A. E. ftpum.
XHMHHECKHR COCTAB MHHEPAJ1OB 113 HlABHblX THflOB IlOPOA/APXEHCKOro KOMMJICKCA

,

OKIKJIM

SiO,

TiO,

Al,0,

Fe,0,

^i

FeO i

I FeO 5

MnO J

,v

MgO 3

CaO *

Na,0 V

K,0 * 

H,0- <^

H,O»-

n. n. n.

P,0,

F

Cy M M a

C y M M a

 Q f ^y^t^ fZZC /

C><ftKte- ?k&/«tl*4!

bHOTOT-njarndKJnMjiuA

rncftc; c BPM^

* v» t i f £ «ui'H* VIA*

B HOT MT

:w oc'i*

fa'aftf*

34,40

3,05

18,71

21,26

0,43

8,64

0,18

0,27

9,25 

>He onp.

2,88

He onp.

99,77

njurnoijiaa

38tt»:i

f/ltfejilt

62,04

He o6n.

23,69

He o6n.

 

.,-

"5.05

8,73

0,13 

He onp.

II M

 1 II

99,64

&«rfMT-M"i!wM»Vo*M4A

ritcftc 

§ y\ 1 1 * S

BlIOTIIT

. w :w

Qiofi/c

37,93

2,36

15,50

19.56

0,28

11,13

0,17

He oT>M.

9,77 

He onp.

2 93

He onp.

99,63

n4ar.iox.ia3 :«:n?J 3

Ph$'"l»"

61,65

He 0611.

24,06

He 0611.

ii ii

n i,

 I n

 n

5,42

8.71

0,12 

He onp.

M II

99.96

riiipOKrciicoAepMamtin XM<\m(niA\tT (AayKpllCTajMIPICCKtlfl C ABIICIl)

PiincprTcti

;ifi 0 15

H^f<f J i\C\

53,26

0.82

0,30

He oOn.

He onp.

19,77

0,(»G

24,76

0.44

He 0611.

He onp.

..

 i

100.01

AIIOHCIIA

116 ii ir,

e

52.28

0.20

1,87

He 0611.

He onp.

6.79

0,14

15,11

22,72

He 0611.

0,08 

He onp.

 

99,19

Pitrnnan

llftMitllK*

.'1? .'Mf.l

HftfvvU^di

40.50

2.10

1 1 .50

6.H4

16.62

0.38

6.50

1.0.51

I.'JO

He uni

1,7'i

He onp

He onp

O.I a

90.50

0.05

99.45

n$?,oK.\* 1

.'Hi OI-1 )

55.-17

llc

0611.

'28 . .'I )

lie

o5n.

. .

He

0611.

. .

I0.'2<)

5.55)

0,10 

llc

oi'p.

.

,,,H

*A

^ ' BtlOTMt'llJiftftli #*!!!& f&to

c UfMJ*- f £.

 J.I K rj

G»^t-\

37.63

He 0611.

20.67

0,83

26.76

1,17

1,43

11,27

He 0611.

He 0611. 

He onp.

99.76

BlIIITIIT

L'.'I H'. r,

fe.'c+iH*

35.50

1,88

I9.K2

1,14

17.25

0.14

11.43

0.05

0.30

8,40 

O.HO

3.39

He onp.

0.20

100.30

0.08

100.22

lUimoKj

'."J .S 1 -1

fUyx.!*

60.41

He odi

24.87

lie o6n

He 061

1 le 061

1 Ic 061

6.61

7.86

0.05 

He onp

«.

 i « 

 

99.81

CO

V6-/V1 --
Ofi'cLt?

OKIKJU

sio,

TiO, \

AljO, ^

Fe,0, 5

FeO v?

2 FeO *

MnO

MgO V

CaO £

Na,O «-

K,O

H,0- jn. n. n. ^

PtOs '

i- 5

Cy M M a i

 O»2F £

CyMMa ^

^

\

«:

A

G-^vv^f

PplHIT

24945

38,21

0,17

21,03

0,85

23,95

0.58

3.96

10,98

*He o6u.

n ii

r

ile onp. 

it

99,73

AMcfutftOAHTOBl

AM<t>ll6cM

/^H^liX*'

tiotVstal-«s*X4.

Puronii

V494S

44,70

0,83

10,79

4,60

13,98

0,27

9,74

11,59

1.33

0,48

He onp. 

2,01

He onp.

0,05

100,37

0,02

100,35

< f t^t^i'e.

HT

b^d//e

Gr<rt«H

BIKITIIT

:-4 045

34,74

2,45

19,50

He 0611.

He onp.

19,72

0,04

10,31

0,36

0,20

9,19

He onp. 

3,23

n ii

99,74

0

PI 'DC****

\\jtniioKjtt3

1M U45

59.85

He 0611.

24.81

He onp.

He onp.

He 0611.

 I n

7,06

7,72

He 0611.

He onp.

ii n

 

99,44

^"CJf,,;.!

/ ^

*Pp*H«T

MWl

37.00

Ho 0611.

20.99

He onp.

32.33

5,80

2,04

1,85

He 0611.

n ii

He onp.

ii 

100,01

M "CM HPM>*

torn v

EllOTIIT

^1 -JOO

37,58

1 ,(>8

16,18

He onp.

He onp.

12.32

0,31

17,99

0,23

0.91

9.07

He onp. 

3.85

He onp.

100,12

fUM

un nu-fic

6/w ¥

fl»*/oC/»^

RjniriioKJI4.1

1'3 '.*)<>

62,23

He 0611.

23.21

He onp.

ii n

He 0611.

n n

4.54

8,98

0.08

He onp.

n it

99,04

3lllUUT 

' " /t /wAA.

UllOTIIl

fo<Q*rf<

G-»r»v*^'

j< &k>

36.92

He 0611.

20,90

He 0611.

30,90

8,23

1,75

1,37

He o6H.

He 0611.

He onp.

ii it

100,07

lM<i>ll6v>jlHTOB*l

- f C*-frfOC£-V.

£>/()// /

BIKITIIT

'.-6 46f

38.86

0.75

17.02

1.90

10.96

0.09

16.15

0.09

0.19

10.00

0.64 

2,80

He onp.

"0,17

99.72

0.07

99.65

4>iu.Hi

I rucftc

tt A^*^C»'/

f(*-*\t'pfljiiriioKJI»3

66.03

He 0611

21.44

He onp

i> it

He 061

He 061

2.67

9.80

0.04

He onp

i. 

99.98

CO

en

AIIIAMTHIM A. U. rc|)Maii. K- K. rywCap. P. 4». llcipona. -.+ 

* liowep
Table I. 6 Paleotemperatures of metamorphism, determined 

from mineralogical geothermometry

EHOTHT-n;iarHOXJia3oBWC rHcAcbi c BUCOKOrV1HHO3eMltCTUMH

MMHepa-naMH

* '*. lr\ - *Lu rr\ i yj ».

5iiOTiiT-n.iarHOKJia3OBbie rneAcu

26431

26339

24301

(Jwooji-iuanioKJiaaoBUe THCflCW

UXHC aM<J>HO'CWHTM

aaynnpoIUHC

:^-S2

24271

24 287

22730

23873

36045

38166

37615

24945

26176

38133

. »,(j

FpaHar 6HOTHT _ 

/C^-0,10; /fjJ^-0.50

/C.5^-0.08: /C^-0,49 

njufeoviH:- Ws.'e^rtf* 

ycxoBHT OHOTHT .

r

U.'ov.tc, 

OHOTHTj

MyCKOBHT 6HOTHT

9

TpaHaTi CHOTHTI 

^-0.25:^^0,54

CajiHT pororfas 

L 0,54;

-O.TO; /fSjlo.54

»AHOOTHT porosan

0,0,97;

.

CajiHT porosaff o<5waHKa 

/CSI-0,66;

Jir*^«.4- <*<

rbaHAT OHOTHT .

/Cjf/S.0,22; /C.^-0,43 

PoroBa* cxSvaHxa ruiarHO

OO*M a HX a IjJiamo

KJtaa

-0,79; /C5.-0.28

Ha.lbHblH

cpii3M.

6o,1HTO83H

To

^ ' *XrO V

fpaHJiTJoamiH

G- ' '

MOp(pH3M;

cpauHH 

To

PerpeccusHufi MCUKH

avid)ii<5o-

 f*

750 \

- -r

PeraoHa-ibHurt 

xop4»«3M; rp

TOB3H d>auilfl

PeniOHa.TbHbiA

MOptpl

roaafl

PernoHajibHwA MCTa- 

; rpany.iHPerMOHajibHbift

MOp4>l(3M.

PerpeccttBHUfl vceTaMOp<pH3M,

UHfl

550

700 

650

1200

ICO

1000

500

36
Geochemistry and Environment of Formation of the Precarnbrian Complex 

A systematic petrologic-geochemical.study of the Precambrian complex in 

the Kola Superdeep borehole and the surroundings was conducted by the method 

of layer-by-layer synthesis and analysis, involving the documentation and 

testing of various rock types, delineated from core logs or from direct 

observation of cores and outcrops. At each level unaltered or only slightly 

altered metamorphic rocks were described together with the variability of 

migmitization or metasomatic alteration and all types of secondary veins. 

Intervals of similar rock types were organized into groups to establish their 

petrographic and geochemical characteristics, the parent rock type, and 

compositional variations due to differences in depth and the intensity of 

metamorphism.

A stratigraphic description of the SG-3 borehole and its correlation 

with the surrounding surface rocks was carried out: chemical trends related 

to magmatic or sedimentary differentiation, or metamorphic zonation were 

studied, and also the relationship between geochemical and the elastic-density 

characteristics of the rocks - in order to determine the nature of 

inhomogeneities of deep-crustal zones.

A. Pechenga Complex

In the interval from 0-6842 m, the Proterozoic Complex is divided into 8

formations:

0-1059 m Materin formation

1059-2805 Zhdanov

Tholeiitic metabasalts, including 

olivine, normal, and alkali-poor 

metabasalts, with minor metapicrites, 

metapyroxenites, and metaperidotites. 

Corresponds in both composition and 

structure to the Quaternary g/cj 

sedimentary strata exposed on the 

surface; broken down into four 

rhythmically layered members: 1) 

2619-2805m gravelly sandy; 2) 

2155-2619m sandy-silty; 3) 1203-2155m

37
2805-4673 m Zapolyarnin

4784-4884 m Luchlompol 

5642-5717 m Kuvernerinyiok

4884-5642 m Pirttiyarvin

5717-6823 m Mayarvin 

6823-6842 ra Televin

tuffaceous-silty 4) 1059-1203m 

tuffaceous-pelitic

Largely (95%) composed of tholeiitic 

basalts, including olivine basalts, 

normal and alkali-poor basalts, with 

subordinate meta-tuffs and 

metasedimentary layers.

These formations are similar in 

structure and thickness: carbonates 

in the upper layers and 

meta-sandstones below; carbonate units 

are largely dolomites with minor 

sands; terrigenous units are arkosic 

meta-sandstones with minor dolomite. 

Meta-trachybasalts (32%), 

alkali-basalts (25%), 

trachyandesite basalts (25%), 

olivine and picrite basalts (10%), 

andesites and trachyandesites (7%). 

Normal andesite basalts (97%) 

Intensely metamorphosed gravellyplagioclase-rich sandstones

On the basis of geochemical data, two stages were delineated which show a 

sharp change in the geotectonic regime during the development of the Pechenga

Complex. The Televin ^formation reflects only terrigenous processess; the *"» > 

Kuvernerinyiok and Luchlorapol formations reflect terrigenous-chemogenic

processess, and the Zhdanov formation - terrigenous processess with minor 

terrigenous-chemogenic processess.

B. Archean Complex

The Archean Complex is composed of plagiogneisses and raigraatites (66%),

araphibolites and araphibolite schists (30%), and granitoids (4%).

Conditions of Formation

The development of the Archean Complex can be divided into two major stages:
first stage (greater than 2.8 billion years) was characterized by the 

deposition of terrigenous and silicic-terrigenous-volcanogenic^ sediments (70%

of the thickness of the SG-3 borehole), emplacement of tholeiitic Basalts \

(23%) and the injection of comagmatic basite-ultramafie intrusives (7%). The 

second stage entailed metamorphism to the granulite stage, followed by 

retrograde metamorphism and ultrametaraorphism to the andalusite-sillimanite 

stage. The metamorphism was accompanied by migmatization and the emplacement 

of veined granites (initial melt temperature 820-830°C) and plagio-pegmatites

(inital melt temperature 810-675°C)

39
nrodoi

u

3

a

>, 9-

t

» 

£

TJ

^

3 

3

7

u 

£

5

\;

a>

<e

r«.

<0

ic

 ^

ri

J

r

*

c

X

s

X

^

^

<<

35-

J <

a

: 

u

C

z 

3

^ CMrtr^f^CMf^oocMOCMOCMO o^Ch-h-CMocnxirtirtcMCMC*

crjCMO OOUOTOOOOO-V Oinaomr^-CMOCMOiTir^- .* _ CM n

"a- CM CM O CM OO X O <OO T tO 

*» aO'S'CMCMOCMOCMCMCMf1^ GO O CM O <O O

^<«5ao»nOOCMOOOOOO T |O»O^ f-f-O | | , | I

CM

tt O «O O O V <»3 V C4 O OO O « d C< i O't'OCJO ' O'voe^ coc*j oior^'rOO o

<«5 i/3Cs"--OO'<O O'o'oo'o'o' O* «» " <M* rt O -J V O~ 1 1 1 1 1

! >. O 30 C< « (O O O T 3O Ifl O OO OO O

otfjo-vao ^«fjo -wo c^mc^f-jcoino-^or^x-vo

 <» oocMtrtoaooo O O O »n CMCCO or^-OfJ'OO o

 <» C-3CSCMO t-O-J

Cv<O^'>~^*rtU5~*OO^Oi'9t eOO ! 

ejSlfit^f^-WIO OOO'WOCM <T5 OOO5'^'<*5OOlrt !

e*5~ o" o'o <N" co*o o'o'vn i n" i^-" irf n" o r«." « " 1 i j I 1 |

Ifl » 0 X « (M ' ! 

O4 !

i

r«« oo oaGt-^o-w vn (^ o<M-wc*3y3OC^Tm -ir:o

r-T V O eToi c^'o'o o'co* d" o c^" «i irt erf dm *rt^ n

 f^oaccixJMCvtirtOJ o m ao ooo ^pOc*50-rorMCM-. 2 o o»oxoxv:c=xr;i^..-^r5

e; o o" o o ac x o" o" t-; V o" o" o '-^ x rt c c*s 1-~ ri 003 

 CM ^ o nr-^ac 

n

OirtiSUtOCJC^lOOOXO-vO O

oonxc'j'^'xoof oo c^ noaoo ni/rro f-^ot^o^ui oo o ut c-J n oi c^ W | ' ; 1

 W <M CM iS (M '

^r»rt oOut^-«'^-cir«-r^.;sox O O ;SC>ir^-«>-'.JOSOi.":;3CMOC: X^-v«<7CXr>--«ri.':ot r>->.T

CM'O'USO" OCrtOCv»COO" OOf*5Ci"'r;cM Ol~- CMO 

o df.TfJr'J'MrM rj 

«

o c« c>i o o> «/5 c» v * o» CM -"t- o> so r-.r^t^CMf^o vciri'^5 ;som oox'rv.t-vxi^'r'-rr'-x-w

 <r^o"oc V o o" »» o" o" o* o" o oo" n £ vrs ^ ir:" n wr: LTS" c^ 

r^> ocvjo CM MO r«.

«oo«oo»u5^5O'O'^'eMOCMOo wiDwoo-fl-wuj-o-vxcMf-j «or^csirrivro--r-<9'f-5x

Vo"«o*Ot^'o"'cicM oo 0*0 o>" irf oi" -.5 x c^j" o r-. vn CM

f- <M<MC3OfO 04n

/

c^c«'iMC<rt«oes«<1*i»rtoo«oo«o CM ocMCSr^ oiC«*3Oooo o ooooootno r~ o r-

 O <^ O C5 O r5 CM O O O O O ^r o" ir; O5 O t>T CM" <» c*5 

r* oor-.xi^-iflcMCMO 

m

1

e

QoS^iS^qqo-qqJl^.^ = . a = a . !

wj H < -<<.(JZiC -'J "Tco^^y^^^yT^^-^ -J^^;>. :

40
6C

9' 

Z>9Z

C7Z

Z'I8I

1^

9'9

O'C

GI'O

9'9

O'Z

E'IZ

Z'9

9'S

67

S'GSE

I'GOZ

Ot'O

it

>

O'll

Z'l

0'09Z

O'OZZ

Z'ZE

0'69

OI'O

0'09

o'e

\'z

9'ZfrZ

O'OC

GZ'O

IT ~

6

es

*>

G'l

e'gei

0'896

97CI

 r'osoi

lO'O

6'e

8'zoe

6'C9Z

l>

, 

G'l

G'81-

~ 

8M

nrodou »nHuiicX<|'|l>c **3W''Y3

Zl

Z'H

I'OI

97*2

979E

6*6*

Z'9ZZ

OI'O

8'*-

e'e

e'z

l>9

8'9

Z>

6>

9718

G'ZZZ

9'EIZ

09'0M

\l

Z'ZZ

O'S

fr'993

9'ZOZ

ne

8'I8

ZO'O

O'S

0>6

Z'9

z'z

O'OJZ

o'oei

e'oez

 ' 9M

mi

69Z

9'OZ

07

9'ees

Z'GOZ

o'9e

80'0

z>

9'S

9'S

e'oz

z'ze

z'e

Z'9

I'lZOI

E'S9I

8'66I

OZ'OsM

8

Z'Gt8'6Z m

9'es

88'0

K9I

90'0

8' 

0'2

Z'9ZII

8'ZI

6'1-ZI

*>e

o'e

0^0

ee'o

z'\

OI'O-r

2C

071

E'e

0'I9I

y'yoi

8'GZ

9'ZZ

90'0

Z'929 

8>OI

z'zei ,

G'l

Z'QL

s>

E'SM

6

6'9I 

z>e

,

9'9I

Z'\

G'801

6'«EI

SO'O

ri

6'86

9'e

Z'OI

fr>

I-'GIS

Z'8^

6'8Z

OZ'O

O'S

OZ'O

IT

£

ez

Z'OGI

O'OfrZ

8'8I

9'ee

69'0

e'is

ZO'O

o'u

^'e

9>

0>

I>OS

S'9

ns

9^0

1*9 n

0^0Ir

E'9I

Z'¥

I-'OGL

9'09I

*'ze

Z'88

«5l

SO'O

6'Z

O'Z

^'5

0>9

s's

o'e

07

0'98S

O'GII

9*161

OS'0H

/V

nvoduu 3niih<)v«X)i(iovv p

ITMVi
-

<

u

5

UJ

X

e; 

O

O

c. 

C

o 

a.

=

V

Z

>,

A

 e-

<n

Hi

^*

Cl

'

O

fc>, 

KOMflOMCHTM

B

C

^*

S5S88Z5!S2?!:§gS!

00 cOCMCnOCOOCO OOO 

CM to t~- CM in co T ^ CM -«r CM 30

C-J~" "*" "<r ""

f- oo o in * CM o »n co co o up CM

in ofo V«o CM'O o CM o" V

3£S*-=S2gg::S:£S23

 w o oo ac o in » » co o o o 

^t^O^vncOf^-COCflCOCMOOCMCO 

CMCM^-O>3OCMO>30O^CM CM

" - ""* °*

gS§?S£8?53S32SS

0 _«-

OCO OOOCMirtOO»CMCMO«3 

OCOOOSOCO COOCOCMCOCMCM

 * -" - -

<400i oeinoooott*.

I>- COCM O'OOCMOOOOCO

tfl o co «r o» o ao o co i>» ao co «r f^ 

aooaocooo mcMO CM co

OCMCM«rO»O3OCO OOOCM

>a 

C*1! <O ^O **^ T*^ O) ?O CO C3 O^ Ol * C*5 ^* 

t^-« OOOi *OJO>CMC4OC^I C^l

" " 

f*» *^ CO '^i Oi O OO CO tip r*» "" CO CO ^* 

O«rO>f«~CMCMCiaOlOCO C5OW3

to 

e

o in t- o o o ac u- vn - m

o ^ Oinmdoacin 

 « f»3 o on o

r>- co " * in " " *n CM Cw wi CM ^r*

 in CM ^ *" co ao

co ^n ao ao m o ao in<o c en

o" <xT oo" co" t>- CM* co" CM* o in" in

 030 CM-9"*-

So-N^OPOrt^O-NCn

O* co o" CM if; o ^r ao" cr> CM co"

in oinin oiocM^in m

 co CM o5 o co o

o cM3oxnocMrMf-«^rx

CM

 oocooo omcMOCM

OooCMCM^rOscomo ^r 

 o in CM

 ^"mo CM U

o o oo «r o m co co

o V so m co 10*0 1 1 1

"" CO CM t>» 

O^rO t^OOCM^rcoao

 « CO 00 CO CM

y

omooomoo o"cM*»o"in'Q"f*"co"o' 1 1 1

 f«. O CM 

CO

 CM

CM CO

CM CM

m oo

CM CM

ro o

o o

O T

CM CM

f^ CM

 CO

I I

 *r ao

1 1

w*2

42
o 

c.

e

iy:iiiuilMc

 eo

*

u:

9

rUH9HOUNO)f 0-

S

-

 e

O TT v/3 

Or- Tr^rsiC?* ."» * O r-O'OOO

O lO O OC 04 TT CM f^ O 1^ <T3 O CM CD 10 co 00 CM CM <-3 co 

 CM

O O CM CM O

=-»»s« ssis-sossss

o oc

O* *o" | CM" irt" CM CM" CO O c*; o" o" oc CM" o 1/7" r~"

*** So CM T*'

o O c*5 r^

o* c"5* O -T" CM* O* c*) GC t*^ O no O O c"

 " CM CM

or^ r^-oc^icDoeno-roo ~ o

*"" 'T ^ OOO CM CM OO 

CM U5 

O oo CM CM ac

 o o oc o L- ,£ ci CM o o i-t cr. c*; c*3 «« rt

 CM

O ^r ^ CM £ ^

"~ -V *~i^OCM° XO^'O 

 CM CM

O o ro ^ m oo

O OO VCMC'JOCM O CO !>. U5 

 CM f*5

O> UO O 

. . .f^tOt"" '9i OO'9> OOr^f>~'9> CMSM

I o CM J CM"O <o"oo"o oc o oco* V

1/3 OC (O GO CMCOOO 

^r CM CM CM

OOOO CM CM 

(COOCMO^f* 'CMO^l/5 aO^OC~*COO

 z; *~ CM ^<-

U3 O 

| J | 0*0* co j o" | o o o PO" m* 0*0*0"

-J H D O t\j «« Z 2 IL. CJ tsj <: n. S i> u u ~z.

oo

ID

»» 

CD

o

CM

00 

CO

 

CM

o

o. 

c

o

5

-r

u.

i o

«5f!;!

= e * = = =

* 2 -^ .. O 3 e :-- s.:

r C s 2 * :

VI- H " :

C C c, .- i - '

 Plli
Table 1.7: a-Mean composition of metasedimentary and metavolcanic rocks of 

the Pechenga Complex from the SG-3 borehole in the interval 0-6842 m. 

b-components 

c-metasedimentary rocks 

d-metavolcanic rocks 

e-continuation of table 1.7 

f-number of samples

g- 1) quartzo-feldspathic meta-sandstones? 2) arkosic meta-sandstones; 3) 

meta-sandstones and meta-siltstones with carbonate cement; 4) sandy dolomites; 

5) meta-siltstones, some with carbonate cement and sulfide minerals; 6) 

meta-pelites, some with sulfide minerals; 7) meta-tuffites some with carbonate 

cement and sulfide minerals; 8) meta-picrites; 9) picritic meta-porphyrites 

{picrite basalts); 10-13) meta-diabases, plagioclase-amphibolite schists and 

amphibolites (10- olivine basalts; 11- basalts with some ferro-basalts; 12- 

alkali-poor basalts; 13- spilitized basalts); 14-16) 

biotite-amphibolite-plagioclase schists, some with magnetite; (14- 

trachybasalts; 15- andesitic basalts, with some pyroxene-olivine basalts, 16- 

trachyandesite basalts)r 17) quartz-biotite-araphibole-plagioclase schists, 

some with magnetite (andesites); "L" and "N": rocks of the Luostarin (L) and 

Nickel (N) series. Content of major elements in weight percent; trace 

elements in grams/ton; dashes indicate element not detected.

44
I I I I I I I I I II

\ o |j i a |4 j o [5 E to

Figure 1.28 -Petrochemical types and differentiation trends of volcanic 

rocks of the Pechenga Complex:

1-4- Mean composition of meta-volcanic flows by formation: 1- Materin; 2- 

Zapolyarnin; 3- Pirttiyarvin; 4- Mayarvin; 5- compositions of the 

initial differentiates; 6-9- differentiation trends for the neta-volcanic 

rocks; 6- Materin; 7- Zapolyarnin; 8- Pirtiyarvin; 9- Mayarvin (numbers 

indicate the position of the volcanic series in the section, from top to 

bottom); 10- evolution of the composition of the initial differentiates during 

the formation of the Pechenga .Complex, I- zone of rocks with normal alkali 

contents; II- subalkaline rocks; III- alkali-rich rocks. Differentiation 

trends for volcanic rocks of island arc series: A-tholeiitic, Bcalc-alkaline, C-alkaline [62], Numbers added to diagram: 

1- picrites, 2-picrite basalts, 3- basalts, 4- trachybasalts, 5- 

trachy-andesite basalts, 6- andesite basalts, 7- andesites

45
Na 7 0«K:0,V.

Figure 1.29 Petrochemical types and differentiation trends of meta-intrusive

rocks of the Pechenga Complex:

1-5 - mean composition of raeta-intrusive rocks, grouped by formation:

1-Luchlompol (a- mean, b-individual compositions of the post-Mater in Complex),

2- Mater in, 3- Zhdanov, 4- Zapolyarnin, 5- Mayarvin, 6-8- differentiation 

trends for meta-intrusive rocks; complexes: 6- gabbro-werlite syn-Materin, 7- 

gabbro-diabase syn-Materin, 8- gabbro-diabase pre-Materin; 9- differentiation 

trend of metavolcanics of the Pirttiyarvin formation. For further information 

see figure 1.29. 

a- Iherzolite, b- werlite, c- gabbro-norite, d- essexite

46
TABJIUUA

O.-CPEAHHE COCTABbl METAHHTPVSHBHblX OOPOJl nEHEHfCKOfO KOMIU1EKCA

M3 PA3PE3A CKB. Cf-3

- KOMflOHCMTU

Si03

TiO,

AljOs

FejOj

FeO

MnO

MgO

CaO

NajO

KaO

PjOj

CO, H2OH2O* +

-f-n. n. n.

So 6m

Li

Rb

Sr

Ba

B

Sc

Ga

La

Ce

Sm

Eu

Yb

Lu

Th

U

Ge

2r

Sn

Hf

Nb

F

Cu

Zn

Ag

Pb

Mo

V

Cr

Co

Ni

 HHCJIO npofi

i

c

37,85

1,01

3.67

7.51

10,38

0.20

26.17

3,20

0,17

0,11

0,15

0,47

0,41

8,77

0,28

8,9

13,3

5,0

13,5

67,7

4,7

5,7

12,0

21,0

2,4

0,60

2.0

0,40.

U

0,20

U

30,6

6.0

- 1.0

3,4

1022,3

190.7

0,27

15,6

4,9

183,9

1603,5

207,7

2519,2

26

:

c

42.99

2,28

7,07

4,44

12,25

0,19

18,12

4,58

0,37

0,14

0,30

0,20

0,11

7,13

0,44

12,5

8,6

13,0

23,5

12,8

6,5

7.5

17,3

32,0

4.3

1,1

1,8

0,30

1.2

0,50

2,1

55,0

4,3

2,3

7.1

237,9

160,3

0,03

5,0

2,1

184,1

977,0

90,3

1121,6

34

3

«s

48,77

1,54

13.39

2,26

12,83

0,24

6,74

8,22

2,72

0,89

0,14

0,14

0,15

2,04

0,05

10,2

27,1

17,7

108.0

6,9

4,5

18.6

10.4

32,4

4,1

1,6

1,9

0,70

1,0

0,70

0.58

26,7

' 2.8

3,0

9,9

141.3

192,7

94,7

0,05

17,6

0,93

280,7

254,7

58.1

147,3

16

c

47.60

1.69

13,22

3,02

12,08

0,22

6,24

8,88

2,68

0,28

0,15

0,56

0,24

3,67

0,11

19.2

9.7

33,9

75,3

14,6

13,0

13,9

12,5

15,4

5,6

1,4

2,9

0,50

0,60

1.4

48.0

4,7

1,9

3,2

55,1

22,7

144.6

0,03

10,0

1,36

362,0

83,8

50,1

103,0

128

4

C

46.93

3.80

10.41

2,47

14,74

0,21

7,82

5,44

0,13

0,03

0,33

0,04

0,28

7,55

0,09

36,5

5,0

12,5

10,0

9,2

9,0

11,5

2,8

70,0

7,0

10,0

400,0

215,0

0,03

4.5

1,5

160,0

155,0

40,5

115,0

3

5

c

52,30

1,96

14.81

2,17

11,05

0,19

2,64

4,38

3,86

2,09

0,56

0,26

0,41

3,39

0,27

15.1

42.7

67,6

256,7

18,6

2,0

28,1

41,8

51,3

12,6

2,8

' 3,5

0,60

4,9

0,60

1,6

139.0

6,3

4.9

17,6

54,8

396,2

0,0 i

8,5

5,6

48,0

20,1

20,5

17,7

39

G

Yo

n

67.81

0.65

14.74

1,73

3,19

0,07

2,10

2,45

2,77

2,77

0,21

0,41

0,21

1,43

0,15

26,2

115,5

47,2

425,9

24,0

5,0

22.7

39,4

96.9

7,6

1.5

5,0

0,50

15.6

6.4

0,54

186,7

6,3

6,9

7,5

472,2

17,9

35,4

0,14

35,4

1.0

74.7

29,4

17.8

12.5

 27

S" \ 2 MeTtnepHiOTHTU. x^opMT-cepueHTHH-ra.ibKotwf n x.iopnT-TpfMO.-iHToaw* C-TSHUU (I />cp- 

( tto.iHTU, 2 Jiepuo.nnTO8ep.nnTU>; 3 4 vifTaraCdpo-a«30a3u. Mc.iaHOKpaToubie n.TaniOK.Ta.t-aM^Hfx*- 

N .loawe C.IIMUU H ax0HOo,nMTU <3 r»GGpoiiopnTW. -I Hopnrbi): 5 accrKCHToawe wrraraoOito JM.I- 

\ Gam. 6 «Mae3HTO-aauHTO8we xoTanop4>HpiiTW. a. c. n HHTpyaHSHwe Koxn.irKCu (a aoMart-ji-

/ THHCKMfl. C CMHWaTtpTHHCKHfl. H IIOCTM JTCpTHHCKHft). Coa*P>KaHHH ntTporCHHUX 3.1«VHITOB .lailu

( » V «3t»tiiTO«-flpHMeceft B r/T, npoiepK codcpxaiiHii H«

47
Table 1.8

a- Mean composition of meta-intrusive rocks of the Pechenga Complex from the

SG-3 borehole.

b- components

c- number of samples

d- 1-2 - meta-peridotites, chlorite-serpentine-talc schists and

chlorite-tremolite schists (1- Iherzolites; 2- Iherzolite-werlites)? 3-4 -

meta-gabbro-diabases, melanocratic plagioclase-amphibole schists and

amphibolites (3- gabbro-norites, 4- norites); 5- essexite

meta-gabbro-diabases; 6- andesite-dacite-meta-porphyrites; S, pr, po -

intrusive complexes (Pr- pre-Materin, S- syn-Materin, po- post-Mater in).

Content of major elements given in weight percent; trace elements in

grams/ton; dashes indicate element not detected.

48
Figure 1.30 Distributional trends of rare-earth elements in meta-volcanic (a) 

and meta-intrusive rocks (b) of the Pechenga Complex.

1-10 - mean compositions of meta-volcanic rocks: 1- raeta-picrite basalts? 2- 

olivine meta-basalts; 3- differentiated meta-basalts; 4- meta-basalts; 5- 

alkali-poor meta-basalts; 6- spilites; 7- raeta-trachybasalts; 8- meta-andesite 

basalts; 9- meta-trachy-andesite basalts; 10- meta-andesites; 11-15 - mean 

composition of meta-intrusive rocks; 11- raeta-lherzolites, meta-porphyrites; 

12- meta-lherzolite-werlites; 13- essexite meta-gabbros; 14-meta-gabbro

4

norites; 15- dacite meta-porphyrites; 16-17 - content of rare-earth elements 

in meta-volcanics of the first (16) and second (17) tectono-magmatic cycles; 

18-21 - distribution of rare-earth elements in meta-intrusive rocks of the 

gabbro-diabase pre-Materin; (18) gabbro-diabase; (19) and gabbro-werlite 

syn-Materin; (20) and dacite-meta-porphyrite post-Materin; (21) Complexes; 22- 

field of continental and island-arc basalts (a) and differentiated trap 

intrusives; (b) 23- field of oceanic basalts; (a) and ultrabasites; (b) A-C 

trends of volcanic rocks, from [62]: A- island arcs and active continental 

margins, B- oceanic islands, and C- mid-ocean ridges.

49
K/Na 

X 20 10 5

Ca/(Ca«AO

Figure 1.31 Petrochemical differentiation trends for sedimentary rocks of the 

Pechenga Complex:

A- Terrigenous rocks

B- Carbonate-terrigenous rocks

C- Terrigenous-carbonate rocks

1-4 - composition of rocks from/bore-hole SG-3 (a) and surrounding surficial

rocks; (b) 1- Zhdanov formation? 2- Luchlompol formation? 3- Kuvernerinyok

formation; 4- Televin formation; 5-6 - plagiogneisses of the Kola Complex (5)

and their general distribution field (6); 7-10 - differentiation trends of

sedimentary rocks of the Zhdanov (7), Televin (8), Kuvernerinyok (9), and

Luchlompol (10) formations.

50

en 

to

200

100

80

60

40

20

(] Zn

4* 0,5 0.6 0.7 0,8 0.9 1 2 J 4 5 6 10

nry nn? G[> m< (

Figure 1.32 Lithologic cx>mpoaition (a, in percent) and geochemical trends 

differentiation (b) for sedimentary rocks of the Pechenga Complex. Suite

1- Zhdanov, 2- Luchlompol, 3- Kuvernerinyok, 4- Televin; 5-8 - geochemica

trends.
EH/

Figure 1.33 Distributional trends for rare-earth elements in metasedimentary 

rocks of the Pechenga Complex. Formations: 1- Zhdanov, 2- Luchlompol, 3- 

Kuvernerinyok, 4- Televin, 5- gneisses and plagio-gneisses of the Kola 

Complex; 6-13 - fields of metasedimentary rocks of the Pechenga Complex (6- 

arkosic meta-sandstones, 7- quartz-plagioclase me ta-sandstones, 8- 

plagioclase-quartz meta-sandstones, 9- meta-siltstones, 10- meta-mudstones, 

11- meta-siltstones with traces of tuffaceous material, 12- meta-tuffites, 13- 

sandy dolomites and limestones); 14-16 - rare-earth element trends in rocks 

of the Kola Complex (14), Luchlompol and Kuvernerinyok formations (15), and 

Zhdanov formation (16). 1- sandy dolomites; II- silty-mudstones; III- silty 

sandstones; IV- sandstones.

53
r/T

< -

7£? -

-iO

*^r

"" T" I

t i t

Ce

r"

La

4

' ^xX

/, ,

Sm

- Eu

V -""""

~i i i

, ,

J^

X

'X

! 1

">

"^

i

"

i

'

**

**

2 -- -

** 52 56

Figure 1.34 Distribution of trace-elements in the major types of 

meta-volcanic rocks of the picrite-basalt (1) and andesite-basalt (2) stages 

of volcanisra in the Pechenga Complex: I- meta-picrite basalts; lime ta-b a salts; III- meta-andesite basalts; IV- meta-andesites.

54
en 

en

.£»:*>

v5u ^fAcl*$

PNC. 1.35. HJMCNCNMW MHHepa^knoro COCT««« 1k«Ta6ii3aJikTO* nrHCHrcnoro / KOMIMCNCB npn np<>rp*ccn»HO*<\ aoHiuikHOM

Figure 1.35 Variations in the mineralogy of meta-basalts of the Pechenga 

Complex within prograde metamorphic zones.
en

Oi

K 2 0

Figure 1.36 Distributional trends of major elements in various 

petrochemical types of meta-volcanic rocks (a) and meta-basalts of the no

aeries (b) with progressive metamorphism in the Pechenga Complex: I - 

meta-picrites; II- meta-picrite basalts; III- olivine meta-basalts; IVmeta-basalts; V- meta-andesite basalts; VI- meta-andesites.
0 1 2 J 4 5 6 

a 'a. ''''7"

son

HOC

mo

w

Figure 1.37- Variation of water content with depth in zones of progressive 

metamorphism in rocks of the Pechenga Complex. 1- meta-volcanic rocks; 2- 

tuffaceous meta-sedimentary rocks; 3- facies boundaries (aprehnite-pumpellyite; b- greenschist; c- epidote-amphibolite); 4- trend of 

variation for mean water content.

57
Figure 1.38 - Distribution of lithophile (1), chalcophile (2), and 

siderophile (3) elements in various petrochemical types of meta-volcanic 

(a) and in meta-basalts of the normal series (b) within zones of progress

metamorphism in the Pechenga Complex. See figure 1.36 for additional 

designations.
Table 1.9- Physical state and composition of metamorphic solutions at various

stages of transformation in rocks of the Pechenga Complex. A - metamorphogenic

rocks, isofacial folded veins; (1) B- folded retrograde veins

1000

2000

3000

4000

5000

nporp«ccuiH««

AaToreHHue

(11)

ABTOrCHHMC

6000

7000

o_r

c/ 

2600

2-5 ilK

560

BlIOTIIT- BioK-k.

&

O ta 

a: os

6835

rr

v *

Ii

Lo

S

A

is

.2 I

?*

I s±

% < ecT 

3 O 0 =n

< n

c 

z <c

Cl )

H <

7V555' 

SI

-f- *

3 s

J «

\i

59
-3 

U

TJ O

O 

C 

-»->

 rH

C!

CD

XI

. i 

CU 

CDH

rt 

-3 -2 C.^:

-T~ r~

S5I5 

 *iS '

« «T 

= c i_ 

 i i .

-/ ^

?5O

76
Figure 1.39 Mineralogical classification of metamorphic rocks of the Kola 

Complex. Rock groups: 1- schists? 2- gneisses and plagiogneisses; 3- 

quartzites; 4- K-feldspar rocks 5- amphibolites. Stock types: 1A, 1Bsubraicaceous schists (1A- feldspatho-quartzitic; IB- quartzo-feldspathic); 2A, 

2B- raelanocratic micaceous schists (2A- f eldspatho-quartz itic; 2Bquartz o-f elds pa thic); 3A-3D- melanocratic micaceous schists 

(3A.-f eldspa tho quartzitic; 3D- f eldspa thic); 3B - 3C - mesocratic gneisses 

and plagiogneisses (3B- feldspatho-quartzitic; 3C- feldspathic); 4A-4D - 

leucocratic schists (4A- f eldspatho-quartz itic; 4D- f eldspa thic) ; 4B-4C - 

leucocratic gneisses and plagiogneisses (4B feldspatho-quartzitic; 4Cquar tzo-f eldspa thic) ; 4E- f eldspa thic rocks (anorthosites) ; 5A- mica-amphibole 

(pyroxene) gneisses and plagiogneisses; 5B- amphibole-(pyroxene)-mica gneisses 

and plagiogneisses; 6- amphibolites; 7A-7B - amphibolite schists, 

hornblendites, pyroxenites (7A- mica-amphibole (pyroxene) schists; 7Baraphibole (pyroxene) -ndca schists). '

A: quartz , '

B: biotite + muscovite

C: plagioclase + K-feldspar

D: hornblende

E: hornblende + pyroxene

F: plagioclase

61
Table 1.10

Nomenclature of Archean metamorphic and granitoid rocks from borehole SG-3

fpynna Moirpynna THO

* ,, 

ycJOBHoe 

nopodu Ha pn

O.narHoTHCHCW H H n.iarHOrneAcu c BFM: 

rpauaTOM, crasPCUIHTOM, 3HA3-

M3HHTOM (BFM)

H MejiaHOKparoBbie njiarHorHeficu c 

BFM

MeaoKpaioBHc njiarHorHefichi c 

BFM

JleHKOKpaioBue 

c BFM

1A, 5 + 2 A, 6

3B, B 

4B, B

n.iarHorHefichi H rHeA 

cu

^TeHKOKpaTOBbie fiHOTHIOBbie

n^arHOPHeAcu (KB<10% 

KB>10%)

JleHKOKpaTOBbie fiHOTHTOBUe 

PHCHCbl

4B 

4B

r3nHJXOT-6HOTHTOBu

Chl

TOBbie n.iarHorHeficbi

Mea

BUC

4B 

3B

BO-6HOTHTOBbie

cnaHUu H n^arno

rHCHCU

fcjPorOBOo6MaHKOBO-6HOTHTOBbiC

c.iaHUbi

PorOBOO6MaHKO80-6HOTHTOBHC

75

55

TbJ H 3M(|)H-

"6ovioaue

CJ13HUU

cnaHuu

6 6HOTHTH3»pOBaHHbie paaHOCTH

6OJIHTH

TajlbK-aKTHHOJlHTOBUe

7 A, 5 6HOTH3HpoaaHHbie paaKO

CTH

paHHTOHrpaHHThi

arHorpaHHTU

FpaHHTHhie

FpaHOAHOpHTU

62
Key to Triblu I. 10

A)-l: two-mica schists and plagiogneisses with high-Al minerals: (garnet, 

staurolite, andalusite, sillimanite). 

2: Biotite plagiogneisses and gneisses

3: Epidote-biotite plagiogneisses

4: Hornblende-biotite schists and plagiogneisses

B)

1: Two-raica schists and melanocratic plagiogneisses with high-Al minerals

Mesocratic plagiogneisses with high-Al minerals.

Leucoratic plagiogneisses with high-Al minerals. 

2: Leucocratic biotite plagiogneisses (quartz less than 10%).

Leucocratic biotite gneisses 

3: Leucocratic epidote-biotite plagiogneisses.

Mesocratic epidote-biotite plagiogneisses 

4: Hornblende-biotite plagiogneisses

C)

1: Amphibol ites

2: Gabbro-amphibolites

3: Amphibolite schists

D)

1: Fe-Mg-amphibolites

Fe-amph ibol i tes

Al-Mg-amph iboli tes

Si-amphiboli tes

2: Porphyroblastic Fe-amphibolites 

3: Actinolite schists

Talc-actinolite schists 

1: Plagiogranites 

2: Granites

3: Alkali-poor granites 

F)

1: Plagiogranites 

2: Plagiopegmatites 

3: Granite porphyries 

G) Field number as in Fig. 1.39; specific designation of rock also given in

Fig 1.39 

H)

1: 6-biotitized varieties 

2: A,B-ditto

63
50V.

50V.

50%

50«/o

0663%

OK

oB

e LC 

^o

O.YL

3,6 1,8 3,0 4,2 5,4 6,5 0,5 1,8 3,0 4,2 5,4 6,6 7,8 E

Fig. 1.40 Histograms of elongation (E) and pie diagrams showing the 

distribution of euhedral (eu) , rounded (ro) , and angular (an) grains of 

accessory zircon in plagiogneisses of the Archean Complex. Two-mica schists

and plagiogneisses with aluminum-rich minerals: a- series I; b- series III. 

Leucocratic biotite gneisses; c- series II; d- series IV. The relative 

proportion of opaque zircons is indicated by the stippled area; P,% - 

frequency of occurrence.

64
a f

falc]/

a tf

GE>

a S

IflflDI*

60 80 Op. 

Fig. 1.41 Modal composition of migmatites and granitoids of the Archean 

Complex plotted on the ternary diagram albite-quartz-orthoclase [19]: 

1 - leucosomes of plagioclase migmatites and two-mica plagiogneisses and 

schists with high-Al minerals (a) ; and leucocratic biotite and epidote-biotite 

plagiogneisses (b); 2-leucosomes of microcline-plagioclase migmatites; 3-5 - 

Archean Complex granitoids: 3a - plagiogranites, 3b- plagiopegmatites; 4agranites, 4b - granite pegmatoids; 5- granodiorites; late-folded granites; 7- 

porphyritic granites and pegmatites; 8-compositional field for plagiogranites, 

granodiorites (a) and granites (b); 9- projection of cptectic lines in the 

system quartz-albite-orthoclase-water at PH 0 = 0.02, 0.04, and 0.07 

giga-Pascals. ' * 

65
Table I. 11 

Average composition of rocks from SG-3 (6842-11,662 m)

KOMnOHCMTW

.o^c^-h

SiOj

TiOa

AI2O,

Fe2Os

FeO

MnO

MgO

CaO

NajO

KjO

PjO,

CO2 H2OH20

n. n. n.

S

Li

Rb

Cs

Sr

Ba

B

Sc

Ga

La

Ce

Nd

Sm

Eu

Tb

Yb

Lu

Th

U

Ge

Zr

Sn

Hf

Nb

TaFCu

Zn

Ag

Pb .

Mo

V

Cr

Co

Ni

MMCJIO npo6_

fljianiorH«Acu n CHeflcu V\fyci,c

1

62,01

0,68

15,40

1,23

5,71

0,07

3,47

1,74

3,08

3,67

0,07

0,20

0,13

0,90

1,48

0,24

51,1

185,7

6,9

85,0

534,3

6,0

16,8

32,1

26,0

54,0

13,0

4,0

1,2

0,67

1,8

0,25

7,1

6,0

0,50

71,4

3,8

4,2

3,2

0,66

1152,8

40,4

145,7

0,03

21,8

1,1

112,8

216,7

25,7

112,3

23

O

63,99

0,68

16,33

0,87

5,55

0,07

2,88

1,99

3,31

2,75

0,09

0,15

0,12

0,67

1,03

0.11

44,6

131,6

7,1

110.4

295,3

6,4

14.1

23,8

24,0

47,0

17,0

3,5

1,2

0,59

1,8

0,27

5,8

5,0

0.51

. 74.7

' 3,0

7,'e 4 1

0,54

872,5

89,4

89, f>

0,08

31,6

1 fi

115|5

150.7

20,8

67,1

60

3

69,02

0,46

15,23

0,47

4,14

0,05

1,79

2,07

3,58

1,64

0,08

0,16

0,07

1,13

0,29

21,8

82,2

2,6

158,9

230,0

7,7

8,8

20,6

24,0

51,0

3.4

1,0

0,62

1,9

0.29

5,6

8,0

0,50

72,2

3,0

4,1

5,2

0,52

244.4

50,9

52.2

0,05

17.9

1.3

76.9

99.3

14,0

44,2

U

4

64,22

0,26

20,17

0,48

1,79

0,02

0.58

2,42

7.7R

1,48

0,08

0,16

0,05

0,07

0,65

0,09

9,8

34.0

1,1

186,0

400.7

8,2

2.2

29,3

25,0

44,0

14,0

2,1

0,81

0,22

0,38

0,06

8.4

3,7

0.50

98,7

2,6

3,7

2,1

0,19

197,3

25,3

35,7

0,03

20,7

0,77

31,0

37,7

3.8

15,1

15

5

70,48

0,34

15,68

0,51

2,18

0,03

0.88

2,09

5,54

1,48

0.11

0,16 0,11

0,25

0,56

0,13

15,7

54,4

1,8

218,2

403,9

8,1

2.6

29.0

23,0

46,0

19,0

2,1

0,78

0,26

0,40

0,06

9,1

4,7

0,50

104,5

2,9

3,6

2.9

0,24

172,9

15,7

43,1

0,05

21.7

0.81

32,8

31,6

4,6

9,5

130

6

70,96

0,27

15,35

0,55

1,59

0,04

0,65

1,68

5,32

2,80

0.07

0,39

0,17

0,30

0,32

0,75

17,9

95,2

1.0

212,0

558,9

8.3

3.2

29.9

25.0

44.0

13,0

2,3

0,72

0,19

0,21

0,05

8,4

2,1

0,50

69.1

3,2

3.1

2.5

0.12

169,2

17.3

44,5

0,06

31,0

0,80

33,7

43.1

5,3

9,9

91

7

65,05

0,50

16,22

1,14

3,19

0,06

1,85

4,22

4,00

1,62

0,13

0,17

0,13

0,28

0,90

0,07

57,0

126,5

1,9

208,5

232,0

6.2

13,9

30,2

14,0

2G,0

13,0

2,8

U

0,49

1,7

0,30

0,70

1.5

0,52

57,0

4.2

4.6

4.7

0.33

383.5

83.4

71.1

0.11

20.9

1.5

139.2

95.4

19.6

42,8

' 20

fOv. '5-5C > *A C\ f«^C ' ^^f

8

62.28

0.59

17,56

0,57

4,54

0,05

1,94

4,00

4,96

2.14

0,13

0,16

0,17

0.19

0,77

0,08

33,2

123,4

3,9

258,8

421.0

6,3

11.3

33,9

17.0

28.0

13,0

2,8

1,2

0,39

1,1

0,22

1,2

2,0

0,53

60,0

3,8

4,3

2,5

0,39

509,4

26,7

115,3

0,05

20,2

0,98

130,4

44.0

15,1

29,6

32

^Z7

9

64,33

0.49

16,91

1,02

3.47

0,05

1,84

4,57

4,61

1.35

0.12

0,!6

0.13

0.16

0.74

0,07

29,0

77,6

233,5

395,3

6,9

11.6

27,1

0,50

42,9

3,5

2,4

312,1

29,2

95,0

0,04

25,1

0,80

88,9

97.1

17,6

72,3

17

10

51,25

0,37

18,09

1,82

6,90

0,11

8,04

4,23

3,47

4.48

0,08

0,17

0,16

0,48

1,57

0,07

30,1

122,5

4,5

249,4

303,1

5,6

15,8

20,6

25,0

25,0

17,0

3,4

1,3

0,90

2,7

0,34

1,8

2,6

0,69

39,4

3,3

4,1

3.2

0,45

931,9

48,3

90,3

0,07

21,4

1.0

156,4

160.9

26.4

107.2

16

3

NJA-.,^ -- 

****fk>

A: 1-3 - Two-mica plagiogneisses with high-alumina minerals (1- melanocratic, 

2- raesocratic, 3- leucocratic); 4-5 - leucocratic biotite-plagioclase 

plagiogneisses (4- quartz content less than 10%, 5- quartz content more than 

10%); 6- leucocratic biotite gneisses; 7-8 epidote-biotite plagiogneisses (7- 

leucocratic, 8- mesocratic); 9-10 - hornblende-biotite plagiogneisses (9-

66
Table I. 11 - continued

A/vc^UjbrX i-nj -i- &~f* PU> t>ol« ~TC ~3»" K-<S ( 5 (_j V' /^fO , T^> * J>7

AM$tt6ojmTM ti * M *n6oJOBue cjaHuu

11

48,15

2,23

10, 8«

3,50

11.33

0,22

9.60

9,85

1,89

0.68

0,19

0,14

1,53

0.22

17.7

23,3

2.6

186,9

154.6

6,b

44.0

21,3

29.0

58.0

8,3

2.7

0.99

2.0

0.25

2.2

2.4

1,0

73,1

5,9

5,5

5.5

1,8

590,8

192,8

150,4

0,03

103,1

1 fi

188,3

414 6

61.0

169,1

26

,: 

50,01

1,40

14,20

3,10

10,31

0,22

6,00

9,95

2,31

0,63

0,12

0,20

0,08

0,17

1,32

0.11

13.8

17.4

2.0

157.3

119,2

6,3

37,3

2u,9

12,0

27,0

12,0

3.8

1,4

0.73

2.5

0,33

1,9

2,0

0 75

68,7

2,9

2,6

3,2

0,53

428,5

129,2

124,8

0.0?

13,0

1,0

239,1

92,1

41.1

70,1

68

13

49,60

1,64

13,54

3,70

10,09

0,22

6,15

10,04 2.3"

0,64

0,14

0,17

0,09

0,28

1,14

0,11

14,4

17,6

2,0

180,0

138,2

5,9

3^,9

23,5

13,0

27,0

14,0

4,1

1,5

0,80

2,5

0,45

1,5

2,0

0,77

58,7

5,6

2,6

3,5

0.51

273.1

114,6

12", 0

0.06

12,3

1,6

3"! 6

80J

50,8

64,0

101

14

54,48

0,80

14,28

2,37

7,83

0.16

5.89

8,7.~

2,50

0,89

0,11

0,26

0,12

0.35

1.47

0,08

15.3

43,4

2,0

199,3

201,3

7 0

31,8

19,6

14.0

28,0

15,0

3,1

U

0,59

2.0

0.34

2 0

2,2

0,57

55,8

3,4

2,9

4,6

0,34

516.8

72,9

97,0

0,0?

18,7

0,89

182,2

29.6

38.7

76,1

60

15

51,72

0,41

17,57

2,20

6,92

0,15

7,95

9,31

2,02

0,51 0,0'

0,15

0,04

0,78

1,20

O.OG

12,6

10.4

2.0

227.1

167,1

4,7

32.9

22,1

7,0

12.0

8,0

1,2

0,58

0,35

1,7

0.31

1,5

2,0

0.50

27,5

2,3

U

0,27

212,1

35,6

160.0

0,04

17.8

0,78

77,8

10i,8

47.4

160,6

15

16

52,73

0,19

' 7,18

2,90

6,78

0.23

12.21

14, 2«

0,54

0,43

_

_

O.Q8

1.52

5,8

5.0

200.0

35.0

7,0

9.0

20.0

.

-

_

_ _

_ _

_

_

_ _

_

1.0

5.0

6.0

sTo

1600 0

5,5

180.0

0.05

15,0

1.0

83 5

540.0

36.0

790,0

4

17

58,01

0,07

2,12

1,60 5,5'

0.1P

24,85

3,49

0,25

0,08

0 Ofi

0,'l6

0,06

2,08

1,58

0,07

3,5

16,7

1,0

22,5

33.8

4.5

5,2

8,2

0,97

5,0

10,0

0,55

0,18

0,10

0,39

0,05

1.0

2,0

1.8

7.5

2.2

0,30

1.5

0.10

750,0

4,4

115,0

0,02

4,1

0,81

14,2

980,0

95,0

2175,0

4

fpaHiiTonau

18

72,11

0,20

14,78

0,79

2,32

0,04

0,63

2,79

5,28

1,30

0,04

0,16

_

0,07

_

8,4

22,0

0,32

172,0

382,0

7,7

3,3

21,0

33,0

64.0

22.0

3,9

0,87

0,51

0,44

OJ5

18,0

2,0

0,50

114,0

2,7

4,1

8,3

0,16

67,5

39,8

34,0

0,06

27,2

0,78

29,8

24,6

5.1

7,2

5

19

72,32

0,11

15,31

0,28

1,62

0,09

0,33

1,25

4.29

3,50

0,05

_

_

_

0,03

_ _

5,0

73,3

0,56

268,1

1085.6

11,1

1,7

26,7

6,0

9,0

7,0

0,66

0,64

0,14

0,20

0,04

U

1,0

0,50

43,3

3,8

1,6

2,4

0.06

61,1

12,7

23,3

0,04

32,2

0,75

11.9

40,2

3,3

8,1

15

20

72,83

0,15

14,62

0,15

2,14

0,03

0,33

1,02

4,63

3,63

0,09

0,26

0,14

0,46

0,61

0,05

21.8

99,4

1,1

111,8

310,0

8,8

6,1

25.6

4,0

8.0

5,0

, 1,0

0,39

0,54

0,48

3.2

9,1

0,50

61,2

3,2

2,7

Z.8

1,2

417,5

83,0

37,3

0,13

22,9

1,3

43,3

48,4

11,9

26,1

16

21

 "« » 

72.19

0,27

14.24

0.73

1.59

0.12

0,50

1,07

3.30

5.40

0,07

0,22

0,16

0,30

0,29

0,10

15,6

229.1

2,5

81,8

342.6

8,3

2,6

3J.O

62,0 '

138,0

54,0

8.6

0,62

0,97

1,1

0,15

41.2

5,6

0,50

81,5

4,1

6,0

4,8

0,40

213,5

6,8

40,2

0,06

53,4

3,4

21,3

35,8

3,1

12,1

34

mesocraticr 10- melanocratic) ; 11- Fe-Mg amphibolites; 12- Fe-amphibolites; 

13- porphyroblastic Fe and Fe-Mg amphibolites; 14- Si -amphibolites; 15- Al-Mg 

amphibolites; 16- actinolite schists; 17- talc-actinolite schists; 18- 

plagiogranites; 19- granites; 20- granite pegmatoids; 21- porphyritic

granites. Major-element content given in percent, trace elements in g/ton /i

(ppro) ; dashes indicate element not detected.

67
Fig. 1.42 Distribution of trace elements in paleosoraes of raesocratic 

plagiogneisses with high-alumina minerals for the Kola-Complex section (a) and 

associated migmatites (b)

68
 52 56 60 68

Wa/K

72 Si02 ,%

O \2

/

* \4 [_*J5

* IP FT!;:

Fig. 1.43 Chemical composition of migmatites and granites of the Archean 

Complex: 1-3 - migmatites (l-paleosomesf 2- leucosomes, 3- melanosomes) from 

two-mica schists with high-alumina minerals (a), mesocratic plagiogneisses 

with high-alumina minerals (b), leucocratic plagiogneisses with high-alumina 

minerals (c), leucocratic biotite plagiogneisses with more than 10% quartz 

(d), less than 10% quartz (e), and leucocratic biotite gneisses (f); 4-8 - 

granitoids (4- plagiogranites less than 1m thick; 5-granites less than 1m 

thick, 6- plagiogranites greater than 2m thick, 7- granites greater than 2m 

thick, 8- pegmatoids); 9- late-folded granites; 10- porphyritic granites; 

estimated composition of raigmatites from two-mica schists with high-alumina 

minerals (a,) and mesocratic plagiogneisses with high^alumina minerals (b,)

69
- a

0.2L

0.6 

Z6

La Ce 3- ^d S.Ti Eu Gd Tb Dy Ho Er Tin Yb Lu r/T

Fig. 1.44 Distribution of rare-earth elements in biotitized araphibolites (a), 

amphibolite schists (b), migrnatized two-mica plagiogneisses with high-Al 

minerals (c), and leucocratic biotite plagiogneisses (d): K= Bi(M)/p, where 

Bi(ra) is the content of REE in biotitized (Bi) or migmatized rocks; P is the 

REE content in the country rock (paleosome)y the degree of biotitization is 1- 

5-25%, 2- 25-50%; 3- migmatites; 4- leucosomes.

70
X.A -

Ma 

H/7

CA

CTfp

Fir^ir half of figure I. 45

Fig. 1.45 Vertical zonation of metamorphism in the section from borehole 

SG-3: 1-5 - roetamorphic rocks (1- raetabasites, raeta-ultrabasitesf 3- 

raetasediraentary rocks, 4- biotite plagiogneisses, 5- sillimanite gneisses); 

6-11 - progressive metaraorphic facies: 6- prehnite-pumpellyite, 7-9 - 

greenschist (subfacies: 7- epidote-chlorite, 8- biotite-actinolite, 9- 

biotite-araphibolite), 10- epidote-amphibolite, 11- amphibolite? 12- retrograde 

greenschist facies; content of metaroorphic minerals: 13- prograde, 14- 

retrograde stage. Mineral associations of metabasites are shown on the 

composition-paragenesis diagrams for the prehnite-pumpellyite, greenschist, 

and epidote-amphibolite facies; for the amphibolite facies the mineral 

associations of metabasites (above) and gneisses with high-Al minerals are 

shown.

71
Ti J' , 

 SSj

 '-',

*» r

u' i 

a

V.

..' fc^i

J/.

\-&,

^^$

V's

'SSs

a

sr

®;® < 

v

$: %-

«

r«r®

#

®*®

%« ®«

<-i

i I

7~T

; i

 n

( |f |« j

L y . 1^ I 

| o \a | ^ |

Second half of figure I. 45

72
frier- 3 986 M.188S

Fig. 1.46 Lithological cross section for boreholes SG-3, 1886, and 1885: 1- 

metabasites, 2- meta-ultrabasites, 3- metasedimentary rocks, 4- boundary 

between prehnite-pumpellyite (above) and greenschist facies (below), 5- 

boundary for the replacement of clinopyroxene by actinolite.

73
Fig. 1.47 Compositional-paragenetic diagram for metabasites of the 

greenschist facies. Numbers near mineral abr'eviatnions indicate the relative 

proportions of ferrous iron (ferrous/ferrous + ferric).

74
MINERALIZATION

The major ore deposits of the northwestern Kola Peninsula belong to 

the Pechenga copper-nickel sulfide district. The majority occur in the 

Pechenga Complex, but some are in the Kola Group. In addition, there are 

iron quartzites, muscovite-bearing pegmatites, and hydrothermal lead-zinc 

veins.

Gorbunov established that the Pechenga deposits are spatially and 

genetically connected with mafic-ultramafic intrusives, having a primary 

metamorphism and hydrothermal activity that produced rich epigenetic 

ores. Most of the nickel intrusives are concentrated in the upper and 

lower parts of the Zhdanov Formation in two trends, Eastern and Western.

Transverse folding of the tuffaceous-sedimentary rocks and 

intrastratal disturbances play a role in localizing the nickel 

intrusives. The intrastratal disturbances usually affect the bottom 

portions of the mafic-ultramafic intrusives and control epigenetic 

breciated ore bodies.

One of the main goals of the Kola Superdeep, located in the center of 

the Pechenga district, was to evaluate the potential for Cu-Ni ores at 

depth, and this has been accomplished. A previously unknown zone of 

ultramafics and Cu-Ni ores was drilled through in the middle Zhdanov Fm. 

Further drilling indicated mineralization of various types not only in 

the Pechenga Complex but in the underlying Kola Group.

Ore minerals were found in the entire section of the Kola Superdeep; 

pyrrhotite, chalcopyrite, pentlandite, magnetite, ilmenite, and 

leucozene. Sulfides ranged from isolated grains to 50%. Greatest 

concentrations were in zones of pyrrhotite mineralization in the 

tuffaceous-sedimentary rocks of the Zhdanov Fm. This formation also 

hosts the ultramafic intrusives with the Cu-Ni mineralization. The 

deepest 3000 m of the Pechenga Complex contain less that 1% sulfides and 

only in the 6000-6835 m interval do sulfides reach 4%, where they include 

chalcopyrite. The sulfides'form streaks of disseminated grains (from 

hundredths of a mm up to 2 mm), veinlets, pods and lenses, in which they 

are associated with quartz and calcite. Quantities are significantly 

higher in zones of cataclasis and phyllonitization.
Sulfides were found also in the Kola Group. Contents vary: in 

gneisses from isolated grains to 0.5% (1-2% in some specimens), in 

amphibolites 0.1 to 0.3% (3-5% in local segregations), and in

meta-ultramafics 0.1 to 0.5%. ~

IS

Oxide mineralization also occurs through the entire depth, but more

$ A 

evenly ditributed than the sulfides. Opaque oxides range from isolated

A 

grains up to 5-10%. They predominate over sulfides in the whole section,

except in the Zhdanov Fm. They include magnetite, titanomagnetite, 

chrome spinal, ilmenite, rutile, hematite, and leucoxene. Magnetite is 

most important in the Proterozoic section; ilmenite, magnetite and rutile 

in the Archean. Rarer minerals were found see table 119. Types of 

mineralization found are:

1) Cu-Ni sulfide mineralization associated with the mafic-ultramafic

s

intrusives in the Zhdanov Fm. and in metamafites and meta-ultramafics of 

the Kola Gp.

2) Fe-Ti mineralization in metamafites of the Kola Gp.

3) Fe-quartzites within the granite-gneisses of the Kola Gp.

4) Hydrothermal sulfide mineralization in retrograded shear zones in 

metamafites of the Pechenga Complex and in rocks of the Kola Gp. The 

first is of both theoretical and practical importance; the rest are of 

theoretical importance only.

CU-NI SULFIDE MINERALIZATION 

CONDITIONS OF OCCURRENCE

(Details of occurrences mentioned above, mostly in the Pechenga 

Complex)

Types of ore and their Mineral Composition. In the Proterozoic

complex there are three types of ore: disseminated ores in altered

/

periodotite, breccia ores in disturbed zones, and veinlet and 

disseminated ores in phyllites. Lean ores in the periodotites have less 

than 2-3% sulfides and about 5-7% oxides but are upgraded by alteration 

to over 15% sulfide. Breccia ores run from 20 to 90% sulfides. Veinlet 

and disseminated ores in phyllite from 2 to 60%. Pyrrhotite is the 

dominant mineral in each, with subsidiary pentlandite and chalcopyrite. 

Considerable descriptive and analytical detail follows, but anything 

indicative of grades and bondages, of copper, and nickel is conspicuously 

absent.
Genesis

The source of Cu-Ni ores was doubtless the ultramafic intrusives. 

Ni-rich pyrrohoite ores extend only 10.5 m from the contact of 

serpentinized periodotite into underlying phyllites. We suggest the 

surrounding tuffaceous-sedimentary rocks have a massive sulfide-type 

pyrite-pyrrhotite mineralization.

Fe-Ti mineralization in metamafites.

Magnetite, ilmenite, and sometimes rutile occur through the whole 

section. They reach a high concentration in the Kola Group at 8711 m in 

schistose biotite amphibolite and metamorphosed gabbro.

Fe-quartzite

Fe-quartzite (7635 m) has a banded texture, with biotite-quartz 

layers alternating with magnetite-rich layers. The magnetite runs 20-30% 

in 0.1-0.3 mm grains. One sample has accessory apatite, zircon, and 

allanite, which is not characteristic of banded iron formations, but the 

magnetite is chemically pure, which- is characteristic of BIFs.

Hydrothermal sulfide mineralization in zones of retrograde 

metamorphism along fractures. These are found at depths of 6 to 10 km 

in both complexes. Salfide mineralization is thinly disseminated or 

rarely in richer lenses and veins, and consists of pyrrhotite, pyrite and

chalcopyrite, with rarer sphalerite, galena, bornite, molybdenite, r^> 

argentopentlandite, and iegnite, with various gangue minerals.

77
The Kola Superdeep confirms predictions on the presence of Cu-Ni 

sulfide ores at depth in the Pechenga District. It has been established 

that these ores are found in the same geologic environment as the other 

deposits of Pechenga, lying at the contact of metaperidotites with 

phyllites, complicated by zones of phyllonitization. In textural and 

structural characteristics, mineralogy and genesis, the ores are like 

those at the surface, indicating persistence to depth, with a significant 

fall-off at 2.5 km. An important find is the previously unknown zone of 

ultramafics and Cu-Ni ores in the middle of the tuffaceous-sedimentary 

rocks of the Zhdanov fm.

These findings change current ideas on the vertical zonation of 

endogenous mineralization in the ores, and clarify the occurrence of 

various types of mineralization at depth under conditions of varying age.

FRACTURES AND MINERALIZED FISSURES

All investigators have emphasized the importance of fracturing in the 

geology of the Pechenga region. Gorbunov et al., have established five 

stages in the history of the ore deposits:

1) Eruption of mafic volcanics and intrusion of gabbro-diabase sills;

2) Karelian folding and intrusion of mineralized mafic and ultramafics;

3) Change of stress directions leading to cross-folding;

4) Metamorphism of rocks and ores under conditions of brittle 

deformatio-n;

5) Displacement of ore bodies along faults with the formation of clayey 

gouge.

j 

Investigation of the Kola Superdeep core was not able to detect the

entire history of fracturing as determined from surface exposures. 

However, it did offer the rare opportunity to investigate the internal 

structure of the fractures, the relation between metamorphism and 

faulting, and the vertical zonation and quantitative characteristics of 

mineralized fractures.

78
Systematic observation of the internal structure of fractures and the 

distribution of mineralized veins was carried out down to 7 km. This is 

for two reasons: 1) the homoclinal attitude of the beds of the Pechenga 

Complex and the reliable correlation of the sedimentary-volcanic beds 

with those cropping out at the surface, 2) the recovery of core in this 

interval by a straight core barrel, which guaranteed the preservation of 

the core "up-down" and its relative position within a single trip. At

greater depths these data were intermittent, but still of interest.

Fractures and Dislocation Metamorphism

Dislocation metamorphism (alteration associated with faulting) was 

studied in the Kola Superdeep through the texture and structure of the 

rocks and the mineral associations including their fabric. (Fig. 1-60) 

There are three groups of textures associated with dislocation 

metamorphism: banded-phyllitic for sandstones, siltstones and 

fine-grained tuffs; schistose for the metamorphic, pyroclastic and 

intrusive rocks, and finally cataclastic.

The fullest data were obtained from the Pechenga Complex, showing 

increasing intensity of deformation and recrystallization downward.

Down to 4340 m dislocation metamorphism was restricted to fairly 

narrow seams, the internal texture of which is determined basically by 

the original rock. Below this depth, original lithology becomes 

secondary, and all the rocks have undergone a prbcess of schist 

formation, with a regular-' oriented fabric of metamorphic minerals.

79
MINERALIZED FISSURES AND THEIR DISTRIBUTION WITH DEPTH.

One of the unexpected findings was the wide distribution at all 

depths of fissures with various mineral fillings. These were 

systematically studied. Doubtless unmineralized factures exist, but the 

logging techniques were unable to spot these in the outside of the hole, 

and in the cores the only unmineralized fractures that could be 

confidently distinguished were those that were a consequence of the 

drilling and core-handling itself.

Mineralized fractures in the cores were divided into two classes each 

with two subclasses A) lithogenetic or premetamorphic (A-l diagnetic 

fractures in the weakly metamorphosed sediments and A-2 contraction 

fractures in the diabase sills) and 8) tectonic (B-l associated with 

prograde and B-2 with retrograde metamorphism).

Fractures also classified by orientation: Series I) /Wcordant with 

contacts and primary textural elements of the rock; 

Series II) High angle, almost perpendicular to same, transverse 

fractures;

Series III) High angle, at angles less than 30-60 to same, diagonal 

fractures; 

Series IV) Slanting, with a thrust relationship to same.

Fractures were investigated in homogeneous intervals. The basic 

measurements were the number of fractures per meter of core and the total 

thickness of veins and veinlets per meter, as a whole and in each of the 

four series, as summarized in the various figures and tables.

80
Discussion of Findings

In the early stages of the geologic development of a single region, the 

character of deformation varies in dependence on the geothermal regime, 

which in turn involves a more markedly zoning or a more uniform vertical 

profile. Under conditions of low heat flow, shallow-type fracturing may 

extend to great depths. It must be added that 10-11 km is the minimum 

depth of the zone of regressive dislocation metamorphism. Unfortunately, 

its geologic age, and the amount of cover eroded are not precisely 

known. Tentatively, 3-5 km may be taken as eroded, so the zone of 

crushing, fracturing and low-temperature mineralization in the Baltic 

Shield may originally have reached to 15 km.

FRACTURING, PHYSICAL PROPERTIES AND ANISOTROPY OF THE ROCK

Fracturing in the cores was compared with bulk measurements of 

density, total porosity, natural moisture content, open porosity, and 

velocities of compressional and transverse waves in three mutually 

perpendicular directions. A clear connection was established between the 

progressive metamorphism and the thrust-slice displacements of the 

Pechenga Complex along conformable faults. It was established that the 

downward increase of the temperature of metamorphism is accompanied by 

the transition from brittle to ductile deformation, with the appearance 

of extensive oriented recrystallization and neocrystallization of 

minerals, and the development of anisotropy toward elastic waves.

Extensive statistical data we« for the first time obtained on the

~ ' - t 

distribution of mineralized fractures to a depth of 7 km. The important

r ">

factors determining the frequency, orientation and mineralization of 

fractures were determined. It was found that mineralized zones of 

crushing, cataclasis, fracturing and low temperature hydrothermal 

alteration, including sulfide mineralization, extend to depths 3 or 4 

times what had been supposed from general principles.

81
In distinction from the near-surface situation, there was established 

a direct correlation of the intensity of development of mineralized 

fractures not with the porosity of the rock but with the anisotropy of 

the elastic properties and the dispersion of the compressive waves.

82
1SW

1580

1620

1660

1700

X

+1s 

Yl/o

Fig 1-51 structure of a nickeliferous intrusive in Superdeep 3, showing 

zonation of metaperiodotite and of Cu-Ni ore.

1. Massive metaperidotites

2. Phyllonitized

3. Talcose

4. Schistose phyllite and siltstone

5. Phyllonitized /

6. Breccia ore

7. Thickly disseminated ore

8. Thinly disseminated ore

9. Rich disseminated ore in metaperiodotites

10. Veinlet and disseminated ore in phyllites and siltstones.

83
1660

1670

1680

1690

+10 +5

Fig. I 54 Lamellar intergrowth of Pentlandite (white) in pyrrhotite 

(light gray) in meta-ultramafic, polished section, x20, 9674 m.

Fig. 1.55 Isotopic composition of sulfur in sulfides of Cu-Ni ores

AT/,

Fig. 1.56 Sch^istose texture of amphiholite with Fe-Ti mineralization ^

(light-gray). Polished surface x9/10, 8711.5 m.

Fig. 1.57 Banded magnetite, ilmenite and pyrrhotite in schistose 

amphibolite. Polished section x60, 8711 m.

84
Kaaavecmoo IOCUIUH u 

npoxuMto8natvt nonet

Fig. I 60. Distribution of^fractures and mineralized fissures in SG-3.

After Kazanskom and Smirnov. 

Original rocks:

1) sandstone, argillite

2) carbonates

3)

4)

5)

6)

mafic tuffs 

mafic lavas 

mafic intrusives 

ultramafic intrusives

Rock textures:

7) massive and spherical relict

8) banded relict

9) banded-phyllitic

10) schistose

11) catacla.stic *

12) ore bodies

85
\

SL

6005

tlur

AK

72SZ

<yy/7////////////////A

'//////A ^

Y//////////A

9 *7 m?w r>^g

Column Headings: 1) Formation, 2) Depth, m, 3) Original rock, 4) Rock 

texture, 5) Fractures and veins per meter of core, 6) Total thickness of 

veins per meter of core, 7) vein minerals: quartz, microcline, 

actinolite, epidote, chlorite, carbonite, axinite, talc, sphene, biotite, 

pyrrhotite, chalcopyrite, pentlandite, magnetite.

86
Fig. 1.61 Change of texture of deformed rocks at depth; a) phyllitized 

siltstone, b) chlorlte-actinolite cataclasite, c) biotite-amphibolite 

blastomylonite. x!5.-

87
Fig. 1. 62 Orientation of minerals in the Luchlompol fracture zone. 

Black rectangles indicate specimens used to measure optic axes of quartz 

and carbonates, mica poles, and amphibole c axes. Contoured at 1 and 

4%. S indicates schistosity, Columns: 1) Formation, 2) Depth, 3) Rock 

texture, 4) Quartz, 5) Carbonates, 6) Micac , 7) Amphiboles.

88
n JT

Fig. 1.63 Influence of lithology on frequency of mineralized fractures 

and thickness of veins dm) in the four series of fractures. Rock 

types: I gabbro-diabase, II mafic tuffs, III peridotites, IV mafic lavas, 

V sedimentary

89
20 60 24 25 75

Fig 1.64 Influence of depth on distribution of mineralized fractures in 

metabasites. a) Number of fractures per meter; b) Total thickness (cm) 

of veinlets per meter; o) percentage of shear fractures; d) distribution 

in groups 1-4.

90
GASES, ORGANIC MATTER, and HYDROGEOLOGY

The results of studies of gases and organic matter is timely since one 

of the important problems that may be solved by drilling of Middle Proterozoic 

and Archean metamorphic complexes is the connection between hydrocarbon gases 

and other forms of organic matter in metamorphic rocks.

Organic matter is defined as dispersed reduced forms of carbon and 

carbonaceous matter and graphite, independent of origin; therefore the symbol 

C is equally applicable for metasediments as well as for highly 

metamorphosed rocks.

Free gases of dispersed gas-producing zones, gases sorbed on grain 

surfaces, gases- bound in cracks, and gas inclusions were studied. Gasometric 

determinations were made in drilling fluid and thereafter at different time 

intervals. The predominantly uncased hole (after 2 km) allowed the entire 

section to be tested. Gas content in closed pores and in extracted cores 

permitted calculation of the fraction of the total gas fraction in the 

drilling fluid.

WELL GASOMETRY

Drilling fluid was sampled at the well head every 2-10m of drilling. 

The sampling probe was thermally degassed with a GBE degasifier (heated to 

60-70°C), and the gas components were analyzed chromatigraphically.

Gasometry results of the drilling fluid are presented in Figure 1.66 in 

cubic meters of gas per cubic meter of drilled rock. Anomalously high 

concentrations were detected for all components down to 11,500m. Helium was 

used to detect zones of gas permeability. Anomalously high gas shows stemmed 

from lithologic and structural-tectonic properties of the rocks (fractures, 

schist formation, sealing factors)* A lithologic control on gas shows was 

established only in the Middle Proterozoic Zhdanov volcanic-sedimentary 

formation where the concentration of methane was characteristic for the 

metasediments and volcanic-sedimentary rocks at various intervals from 1050 to 

2770 m.

Concentration of associated methane was anomalously high in the 

metasediments, but was less than 20% of the total concentration in the 

drilling fluid. Methane content decreased with depth to 0.05% in the 

Proterozoic complex, and to 0.03 - 0.01% in the Archean (7500 to 11,050m).

91
Figure 1.66. Gasometric results of drilling fluid during 

drilling of CG-3 at intervals of anomalously high gas indications 

(cross hatched). ,

Given are mean values 'by interval (shaded) , dotted lines signify 

intervals where He was detected during repeated gasometry of 

drilling fluid during breaks in drilling operations. Background 

concentrations are in cubic meters of gas per cubic meter of 

drilled rock: He - ...... HH& - 0.2x10"^-.

92
Supersaturation of the drilling fluid by the gas components during 

drilling was observed in the Upper Proterozoic as a spontaneous release of gas 

from solution in various intervals from 1100 to 4570m. Anomalous heavy 

hydrocarbon gas (HHG) contents coincided with anomalous methane concentrations 

at various intervals, whereas their absolute and relative values in the total 

hydrocarbon gas concentration increased, especially after 8800m.

Prom repeated gas sampling of drilling fluid during drilling intervals, a 

number of intervals with increased gas shows indicated by helium could be 

classified as dispersed and gas permeable (4800-10,750m).

Helium content of the rock based on gasometry data from the drilling fluid 

is presented in Figures 1.67 and 1.68; this identifies the fraction of bound 

helium released from the rock during drilling, which did not exceed 10% in the 

fluid-permeable zones in the Proterozoic and ranged from 30 to 100% in the 

massive rock. In the Archean gas-permeable zones it ranged from 0.4 to 4%, 

and 10-40% in the relatively impermeable blocks.

The information content from the carbon dioxide after 8800 m is balanced 

against the addition of sodium carbonate to the drilling fluid at 8700m; 

however, the spikes of helium, nitrogen, hydrogen, methane, and HHG indicate 

that the carbon dioxide content is not simply due to contamination.

GASES IN ROCKS

Studies of gases in the closed rock pores in Kola Drillhole SG-3 are 

applicable in solving the following problems: establishing a relationship 

between the distribution of gases in ancient crystalline rocks of different 

origin and composition as a function of depth and geological setting; 

determining the role of the gaseous phase in the processes of endogenic ore 

formation and metamorphism from prehnite-pumpellyite to amphibolite facies 

with active granitization; establishing the gas fraction in closed pores 

relative to the gas content in the drilling fluid to identify fluid conducting 

zones and also the specific gas content of the roc/ks.

The principal characteristics of the helium and hydrocarbon gas (HG) 

distribution in SG-3 shown in Figures 1.67-70 are:

1. A decrease in total HG down to 4884 m; and subsequent stabilization 

of the average values with second order variations depending on rock type and 

classification as formation or strata. For example, the metasediments of the 

Zhdanov Formation are distinctly different from the extrusive and intrusive 

Proterozoic rocks; a strong reduction in HG for metasediments at the
SEtWk V

o « o« o

 ' V V"Tg

" » 4 « * «

o o a a 

o a o

V V VV

V V V

LULL

r r r r

r r r 

r r r r

.-..

r

r r r r

r r r r 

r r r

2.5 75

1000

1500

2000

2500

He 

/ 0,3 7,5 17.S

J5

1020050,1

0,3

0.5

tojs

Figure r.67. Concentration of helium, methane, heavy hydrocarbon 

gases (HHG), and C cr^ in rocks of the Pechenga complex in section 

of Well CG-3: 1 - augitic diabases; 2 - pyroxenic and picritic 

porphyrites; 3 - basic pelitic and silty tuffs; 4 - basic 

psammitic tuffs; 5 - basic tuffaceous lava and lava breccias; 

6 - tuffite; 7 - phyllite; 8 - siltstone;, 9 - sandstone; 

10 - conglomerate; 11. - sandstone conglomerate; 12 - quartzitic 

and arkosic sandstone;' '13 - quart zite-sandstone and quartzcarbonate-mica schist; 14 - actinolitic diabase; 15 - spherolitic 

lava; 16 - diabase porphyrite; 17 - magnetite-plagioclaseamphibole schists and plagioclase-amphibole schist on 

metadiabase; 18 - magnetite-biotite-plagioclase schist with 

amphibole on andsitic porphyrite; 19 - basic and acidic altered 

tuffaceous lava; 20 - orthophyre; 21 - biotite-amphiboleplagioclase schist in andesitic basalt; 22 - magnetite-sericitechlorite schist with carbonate; 23 - dolomite; 24 - metamorphosed 

dolomite, marble, carbonate-tremolitic schist; 25 - chloriteserpentine-talc and talc-tremolitic rocks; 26 - gabbro-diabase; 

27 - gabbro-diabase essexite; 28 - amphibolite with massive 

gabbro-diabase; 29 - andesitic porphyrite; 30 - pocket-streaky 

sulfide ore marifestations.

94
96

aze'o .

EE£

COS'S

oosa

ooos

OQS

000*1

J J J 

J J J 

A » A W A 

A » A 

'^.. A. 

A A A 

A <» A » 

V 1 

o o 

o o o 

O 0 0 

dz
CD
IH

0,223

0,023

0009

0027

urn

mtum 

0,126

0,021

QT

9 V<r » H~tt « /J

Figure 1.68. Content of helium, methane,'HHG, and Corj in 

Archean rocks of the Kola Series in well SG-3: 1 - biotiteplagioclase gneiss; -2 - sillimanite-biotite-plagioclase gneiss; 3 

- two-mica gneiss with VGM; 4 - two mica gneiss; 5 - garnetbiotite-plagioclase gneiss; 6 - epidote-biotite-plagioclase 

gneiss; 7 - epidote-biotite-plagioclase schist; 8 - magnetiteamphibole schist; 9 - amphibolite; 10 - amphibolite with 

cummingtonite; 11 - banded (leucocratic) amphibolite; 

12 - biotite-amphibole schist; 13 - phlogopitic rocks; 

14, 15 - intrusive formations (14 - plagiogranite and dark 

mignatite, 15 - plagiomicrocline granite, pegmatite); 16-18 - ore 

manifestations (16 - sulfide, 17 - magmetite, 18 - ilmenite); 

19 - quartz veins; 20 - chloritization; 21 - microbellnization; 

22 - muscovitization; 23 - migmatized zones.

97
I

Figure 1.69. Helium content in the rocks of Drillhole SG-3.

Rocks of Middle Proterozoic: 1 - gabbro-diabase, gabbro of 

differentiated intrusives; 2 - peridotic; 3 - diabase; 

4 - picritic porphyrite; 5 - andesitic porphyidJte, albitophyre 

plagioporphyrite; 6 - tuff and tuff breccias; 7 - psammitic"" 

metatuffite; 8 - pelitic metatuffites; 9 - metapsammites; 

10 - metapelites and siltstone; 11 - carbonate rocks; 

12 - biotite-plagioclase gneiss^^ schist;' 13 - biotiteplagioclase gneiss, schist with VGM; 14 - two-mica gneiss, 

schist; 15 - two-mica gneis, schist with VGM; 16 - epidotebiotite-plagioclase gneiss; 17 - biotite-amphibole-plagioclase 

gneiss; 18 - epidote-biotite-amphibole-plagioclase gneiss; 

19 - garnet-epidote-biotite-plagioclase gneiss; 10 - biotiteamphibole-plagioclase schist; 21 - epidote-biotite-amphiboleplagioclase schist; 22 - amphibolits; 23 - banded^.large and 

irregularly grained amphibolites; 24 - leucocra^ic amphibolite; 

25 - large and irregularly grained amphibolite; 26 - amphibolite 

with cummingtonite; 27 - amphibole schist with cummingtonite; 

28 - biotite-amphibole schist; 29 - talc-actinolite schist; 

30 - plagiogranite and dark migmatite; 31 - microcline granite; 

32 - pegmatite. Average helium content - center of rock symbols, 

range of concentration indicated by length of line.

98
2 -

Figure 1.70. Total HG in the rocks of Drillhole SG-3 

Symbol designation same as in Figure 1.72.

99
1/1000 1/500 -1/300 f/200 1/100 1/50 1/10

Figure 1.71. Helium content as a function of the concentration 

of uranium and thorium in amphibolite in rocks of the Middle 

Proterozoic and Archean complexes in Drillhole CG-3:

I f 2 - amphibolites of the Archean complex, including 

cummingtonite (2); 3 - amphibolites of the Proterozoic complex; 

4 - outline of the field of amphibolites of Series I (6842-7622m) 

of the Archean complex; 5 - outline of the field of amphibolites 

of Series II-VII of the Archean complex; 6 - lines of equal 

coefficients of retention of helium. Remaining rock designation 

same as in Figure 1.72.

Table 1.29. Average concentration of hydrocarbon gases, nitrogen 

(Cm3 /kg), and organic hydrogen (%) in metasedimentary rocks of 

the Zhdanov Formation as a function of sedimentation conditions.

100
muscovite-chlorite to biotite-chlorite transition zone of the greenjschist 

facies at 3180 ra; and a minimum HG content in the Archean section in the 

biotite-plagioclase/ biotite-amphibole- plagioclase gneiss, and amphibolite 

series (7622-9456m) for nearly all rocks.

2. The helium-content profile is the reverse to that of HG. The helium 

content increases for all Proterozoic rock types down to 4884m (Luchlompol 

Formation), with a tendency for decreased helium content at 10,600m; and is 

also observed in the pegmatites and granites. The bulk of the granites,

however, fall into the domain of low and medium helium content; minimum values o-f 

are widespread throughout nearly all the Archean migmatite and plagiogranite

series.

3. The helium content significantly depends on depth down to 5 km. At 

greater depths the predominating factors become the structural-textural 

properties of the rocks, the mineral composition, the uranium and thorium 

content, the age of the rocks, and their origin and history of metamorphism.

The reduction in the coefficients of retention of helium in the 

amphibolites with higher uranium and thorium content suggests that granitizing 

solutions have been introduced to these rocks. The high magnesium 

amphibolites with cumraingtonite are more resistant to the granitization 

process and hence helium'retention is higher. Plagiogranites and migsTatites 

are more yielding to the recrystallization process of the granitizing 

potassium-rich fluids and hence fall in the upper left quadrant of the 

diagram* (ftg. J., 7/j 

4. Nitrogen content in the Zhdanov Formation reaches 20 cm /kg and

correlates with HG and C

org

5. The direct correlation between the content of C , HG, N0 , and

org 2

the light isotopic composition of hydrogen in HG is evidence of the biological 

origin of these components; confirmed by the dependence of concentration on 

facies formation condition's^

6. The results of gas analyses averaged by rock type are plotted as HG - 

C and HG - He in Figures 1.72, 1.73; and testify to the joint occurrence 

of HG with the bulk of the helium in a single system of pores. The partial 

pressure in a system of connected pores in the earlier metamorphic stages 

within a single unit is approximately the same, and is preserved as such, 

after the pores are sealed. The quantity of helium depends on the total 

porosity and C content. Apparently the preservation of helium as a 

function of depth and leakage of helium from the Archean basement begins to be 

significant.
Figure 1.72. Relationship of total HG and helium in rocks of 

Drillhole CG-3: . . 

I - field of metasedimentary rocks of the Matertinskiy and 

Zhdanov Formations; II - field of volcanic rocks of the 

Proterozoic complex; III - field of Archean. rocks.

Figure 1.7-3. Relationship of total HG and C or~ in rocks of 

Drillhole CG-3: J

I - field of metasedimentary rocks of the Proterozoic complex;

II - field of Series I, III, v rocks of the Archean complex; 

- field of Series II and IV rocks of the Archean complex.

102
7. A connection is lacking between the average content of total HG and 

C in Proterozoic rocks, and there is a negative correlation between total 

HG and helium.

8. There is a negative correlation between the total HG and C in

org

series I, III-, V of the Archean complex; and no established connection 

between these components in Series II and IV. This lack of a connection 

between helium content and total HG is characteristic for all Archean rocks, 

due to the discrete nature of gas sources and the forms of their occurrence in 

the rocks.

9. Carbon dioxide and HG are the principal gaseous components of fluid 

inclusions in quartz, the rock-forming mineral in hydrothermal veins and 

pegmatites; their content is higher in metasedimentary rocks. For Archean 

series the principal component is carbon dioxide in quartz of hydrothermal 

veins and pegmatites, but HG is nearly absent. The granitization process is 

accompanied by an increasing fraction of carbon dioxide in the fluid phase 

which participates in the formation of hydrothermal quartz-carbonate and 

carbonate veins in the Archean and Proterozoic complexes.

Regarding the connection between the gas phase in rocks and ore genesis 

the following facts are emphasized: 1) helium inflow was detected in the 

interval 9950-10,500m during well down-time; and during drilling anomalously 

high concentrations of He and HG in the drilling fluid were associated with 

high concentrations of helium in the.cores. Apparently this interval is a 

zone of weak ore control .and poor fluid permeability; 2) the ore-bearing rocks 

of the Zhdanov Formation are distinguished by increased HG concentration in 

rocks similar in age and composition to other regions, which can be used to 

evaluate volcanic-sedimentary rocks for sulfide mineralization, 3) the inverse 

relationship^between uranium and thorium concentration in Archean rocks and 

helium retention indicates the later introduction of specific radioactive 

components (Figure 1.71).

GEOCHEMISTRY OF ORGANIC MATTER 

' < >

Geochemical studies of the organic matter in Drillhole SG-3 included

quantitative determination of the C in a chloroform bitumen extract

org

(C3E), the elemental and component composition, and also

structural-chromatographic analyses using infrared spectroscopy (IR), electron 

paramagnetic resonance (EPR), nuclear magnetic resonance (NMR) and gas-liquid 

chromatography. Over 500 determinations established the CQ distribution
shown in Figure 1.74, whose concentration varied from "traces" to 2% in 

Proterozoic volcanic-sedimentary rocks, with a maximum in the Zhdanov 

metasedimentary rocks (phyllites, siltstones, sandstones), and decreased to 

0.1%, and 0.01% in diabases, gabbrodiabases, and porphyri.tes. The 

concentration ranged from 0.01 to 0.03% in the Archean rocks.

Rock bitumen content was analyzed by bitumen luminescence; however, at 

high stages of catagenesis the physico-chemical bonding strengths of the 

bitumenous matter with the surrounding mineral medium sharply increased, 

reducing the reliability of the determination.

The chloroform extraction data are most interesting (shown in Table 1.30) 

and establish two basic relationships, namely that Proterozoic rocks have a 

higher CBE than do Archean rocks; and second that the CBE distribution in 

Proterozoic rocks is characterized by a maximum (up to 0.2%) in the 

metasediments, and a decrease down to thousandths of a percent for volcanic 

and volcanogenic sedimentary rocks. The direct correlation between CBE 

concentration and C in purely genetic varieties indicates the syngenetic 

nature of the bitumenous matter. The CBE components vary stratigraphically, 

as well according to genetic types of rocks in the Proterozoic.

The elementary composition of CBE is shown in Table 1.31, and illustrates 

the differences in the Proterozoic and Archean deposits in the distribution of 

hydrogen containing compounds, as well as in their structural properties. The 

latter is reflected in the C/H ratio.

The CBF components of the metasedimentary rocks possess different 

structural properties (Figure 1.75); oil is represented by oxygen-containing 

aliphatic and cyclic functional groups. A separate structural type of CBE was 

detected in Archean deposits; the basic oils are composed of high molecular 

paraffins.

The following were determined: range of the series of n-alkanes, the 

location of the maximum concentration in the series and the concentration of 

"liquid" compounds, the oddness value factor (ratio of total n-alkanes with an 

odd number of atoms to total even number), the principal differences in the 

distribution of the CBE oils in the Archean and Proterozoic, and the 

distribution characteristics of the iso-alkanes beginning with C , (Table 

1.32, Figure 1.76). The predominate component in the CBE oils of the Archean 

deposits are the n-alkanes; a negligible quantity of n-alkanes were found in 

the Proterozoic extrusive and intrusive rocks (Figure 1.79) ; and the 

metasedimentary rocks of the Proterozoic were ch*^*cterized by an increase in 

n-alkanes.
(X

o

Ol

SP ?

o

r

? 1 

r s

<$ 3_ * ftF §1 £

\ fi>

\f» ^

^ CL

'\\

\ ^ 1

' ^

 ^.. *

^ b-

\ «.

* w 

i ^

V ^t

* ^

^ X r--

Q Q.

i "^K

^ °

^ Oj

H- §

^ 5

^ \

~h V

^ Js

^ -

If)

7s S

t " \L

f 4? ^|

r ! I ~ t£

1 o tr

\ s a V .-.^

E s c £ e; ^

j* rt x ^

rt>

O C

8 £

tO t£ 

OO O

O 4.

k.

1 5

i 3

oo <r> ftt

? iz ^» -J jo -n

5 -4 »o o <g M h 1 ~ > oo -^i -^i -~i . " 

j co co cn o vl>

3 tO 4k, Ol 4>. y

> 4k. 4^. cn oo £

1 0 CO j JJ

i -i ) i ^» Vj 3 

"'o.^ og §

st1 ^!- » 1 ft> tf

E t

> oMo \# o J ( J

> gK*?^ 3 J jL

.i ' a \u

5 tC o\ 3 I/ SP ? 

* Oi \5iII.3ren 3t<*

c*l\^ ** Cn x

Vr ! * n

O O /O O O ° j 2 D

o g I go o o i i ^

 to|tO- O 4*iJ ^,

Co tO'j Cn to I fy // 

^ U to cn cn * ^

^1 tCf J tO CO 4k. i °

Cn IO, 1 to Cn |

" N

a i

&J s

P 5

8 f

Uj x\-

^

^

0

'1 JO tO j

I to O cn cn '

f Cn 4>- OO I 

1 IO 4*. OO I

£~ w S j

O ^-1 CO CO '

 cn 4k. to

oO* V) 1

S \ ^

. _ \ ^ \ _

5

C I

ej ^ .

trt 1" C

r r j -J Ol C

cn -^ c 

 ^ -~< u

co \ cn

p-i>acxotrtXijrc._.ii>^iOM.o!«

S8i l3 es?|8J

rtias oaxWa 

paicx w^^Cs

(a Q tr C* . .t

09 f - ' S £ ?

i* U 

1 W 

t I

/4k. CO CO 1 CO

. /cn..to^i icn^

^ / CO^OOCrt 1 41^ Jg 

J 4k. 'o£jCOK> j^tO

N| "^ cncnboi 1 oo 4».

" [Mill

*. t_ : 4k 4» CO CO 1 COCO 

O'Ol -^JCOCO~~I lOltO

n oocooocn ,| o» O

0 4- tO -1 -4 ,1O 

To co 4^ I to

1

oi"

nIO 

to tc

tO Oi 

 Oo

co

"^U^QW i E-e-p'?S»£I'c -oI 

"tsS^gs^fcSS^^g-e-Sf

H O * S3 y ff 5-v5 tr *"* *<'t

J "" »i

" " * ' * ^ ^ 'I g0> 1

O O O O OOOO OO

p opp oooio oo 

4! eri X- J- tooO-4 o> co

to tptoto oo to to 4 oooo 

cn J^-cnco oo 4- 4- 4- to oo

^00

It-1 4^

cn 

MCO

cn

1

13 L

8 i

*. 

1 t

 i

tO 

O 

cn :

o j 

aoSoSC

tf|f|

s x l3 tj n 

EO\E, CXJC 

w "" w 

«S w 

1 

OOOOOjO 

28 CoS]

4 P 

^4- 

> 

Oo OC *^l Oo ' * -*4 

Ocncncoi^- 

O OOOO OtO4-O IOCO 4>-C/«

o o o o oooo oo

o o p p * o p o o o 

 tocnto oocncnto encn

CJ4^^

/\ i 

OOOO.T'O 

8S S8i

en cn to to cn Ci» o« Oioo cn ' 4- f

K3 4*4k.CO >-lOIO4k COtO 4»

o -44i.to ^14-tocn cn4>- 

C> ooooo ooCoCnO» OtO

to to --1 4->> CO 4k tO 4-i COCO

cn t/« 4». to en <o o cn oo co 

to oo oo c« Oienioto ~~j oo

oo aa - 

to -J tt

o 

oi Cn -

-I cn i oo -^i oo -^100 

3 4-. cnCJiCn to 4-

" tO Cn p p cn to to 

 O>CnO4- Cn4-

o cnto^i tocnoto 1000

cn 4»-ocn o cn p tooo 

 to en 4^-oototo cn

" & £

3 _*1 ^

t .*. J1

O POOO oo

 \ { oocn co co

\ _A _. CO 4- -J to

-B

Cn oo --i ~vj

IO4~

to cn ~vj to

toco

a. to

 00-4 

4^ tO IO CO

to to

4- tO

O 4k 4^ CO

to cn

000

10 a

*<

c

4.

F

r

to £

- T

1*

k

oo 

oo 

OO 

8 

C/« 

00 

CO 

to 

CO 

-4 4

4^ 

O C

 "

to 
Qt^*&±SL

~" j 

ftTtS+^J&l 1 ^

HHTepaiJi 

or6op* npo6, u

771,2 771,9

' 1 1 1 QQ n 1 1 QQ 7

t^ 

1199,8 1200.8

i - 1 n n i 7 1 o o

2 63

2166,9 2167,2 

2459,9 2460,5

2606,3 2608.2

2608,8 2610,2

4855,6 4862,9

4863,8 4566,1

M

^n^fi % 90^ i *)

2657,1 2658,7

370,3 373,8

902,8 903,6

1581,3 1582,6

 o / 

IcnCic

-R^~

fv^ta"! \>* 

-r- ff M B T 3 T y t 11

I'Vyfi^peu-HiL ^J - v 

AVe T a n a .T n T « H- <i jr

/* i nn H^TW 11 ro dRvownauif

{ a.aeBpiiTOBbia cianeu H a^eapone.UiTOBbift c-ianeu

/CioiicTuft rpavaaKKOBwA

\ a.iespHTOBua c.ianeu

/ToHKOC.ioiicTun rpayaaKKO-

^V^wac^ti S///3* i*e.iil~e.

L p3V-S3ivKO y it* 3«T£8pO*I!lT 

"^ J f -"^ C J^ *V\ 1 TW

*\*T 6 B y QZXC^l XJ M 1 1 T

^ THT-CepllUHTOBfaJM UCMCHTOM 

/ApK0308faJH nca.MMHT C reM3-

^Tirr-cepumiTOBfaJM ueMCHTOM

i r ii T T ii ,n 'n * it ii n n n p n J__M

TST^HR-vftnboUx. a*iV.ro

JUpww.^^lJ^rte

,no

c

c

d 

65,49

e H p u u« 

71,19

60,41

64,81

55,85

67,68 

55,82

69,90

68,87

55,94

56,44

61,00

70.08

fiQ Q"}

* T p ;i n r H 

68,82

70,29

66.98

H

6,71

.T H r U

10,21

8,66

9,79

7.03

9,40 

8,65

10,53

9,86

8,11

8,14

n r n r n^r

8

tyi

7.46

10,37

9,73

t

S

I'3

8.14

S

I

f\ « 

,3o

0,65

0,0

1 99 .--

0.002

0,95 

0,00

0,00

0,61

0,00

0.00

T 3011 0

O ca

0.00

0.00

0.86

1.28

0.00

1 . _.. ,

* C-f'^wt&AVi

X

0,00

26,45

0,00

17,95 

1.18

29,86

0,00

24,18

0,00

37.12

0,00 

21.67

0.00

35,53

0.00

19,57 

0.00

20,60 

0,00

35.95 

0,00

35.42

bss»\c jVtecp

0,00

30.07 

0,00

22,46 

0.00

19.70

0.00

20,59 

0,34

20,19 

0,00

24,87

roc/cx,

£-3/ cJ f

i06
3uU c^"*2

6475,7 6485,7 

7647,6 7664,1 

7670,0 7677,5 

8460,4 8460,8 

8941,8 8942,5

7120,1 7134,0> 

7771.4-7778^

Ajutuifioaatti/lm^fufcol.^S

A M ((MI 6 u <j fl T U'~ 

69,86

*69,90 

69,41 

63.60 

63,60

8993,9 8997,9; 

8998,0 8999,7

8525,5 8628,2; 

8637,3

9352,4 9355,9

^P-mrfrrHeiicu

SniUOT.fitlOTHTOBbig fHCHCbl 

Crr>e-;*v2. 

-fJIOl'lOIJ74,00

68,89

60,70

63,60

70,60

9,60

9,60

8,22

11,00

11,20

11,90

8,60

10,20

11,30

11,20

0,00

0,00

0,00

0,00

0,00

0,00

0,00

0,00

0,00

0,00

0,00

20,54

0,00

20,40

0,00

22,37

0,00

25,40

0,00

25,20

0.00

22,50

0.00

29,50

0.00

29,50

0.00

25,10

0,00

18,20
I

*i/

ma

tlUJ

mt

S*

ktu

0.01 0,1 . 1

I 1 1 in\ < i i 1 mi ! i t i i i nl

R +

&** '

Figure 1.74. Concentration of c org in rocks of Drillhole SG-3 

Symbol designation same as in Figure 1.69.

108
700 1100 1500 TOO 1WQ

Figure 1.75. IR spectra of CB£ and components.

Middle Proterozoic rocks: I - diabase (1954.7 - 1958.4 m) 

" ' ^ff (3752.1 - 3757.4 m) III - tuffite (765 - 885 m )'; 

IV, V - phyllite with siltstone (1182 - 1496 m) , Archean rocks; 

vi - epidote-biotite-plagioclase gneiss (9600 - 9980 m); 

VII - biotite gneiss (8313.1 - 8324.0 m); a - CBA; b - oil; c - 

petroleum ether resins; d - benzene resins; e - alcohol-benzene 

resins.

109
Figure 1.76. Chromatograms of the n-alkanes and iso-alkanes of 

the CBE oils.

Archean rocks: a - two-mica gneiss (10,144-10,181 m); 

b - biotite gneiss (8313.1-8324.0 m) . Proterozoic rocks: 

c,d - hyperbasite (1954.6-1958.4, 1757.8-1767.6 m) ; e - tuff 

(3752.1-3757.4 m) ; f - phyllite with silt;stone (1182-1496 m) .

110
The results of the geochemical studies indicate that the quantitative 

distribution composition, structural properties, chromatographic 

characteristics of the CBE organic matter depend on the formation conditions 

of the different genetic types of country rocks. The geochemical 

sedimentation setting was favorable for the accumulation and preservation of 

organic matter, which upon transformation generated bituminous aliphatic and 

cyclic components. Intrusives probably assimilated the organic compounds and 

transformed them into a variety of organic systems at high temperatures.

Since petroleum was added to the drilling fluid below 7 km, special 

studies were carried out to determine the contamination effects using 

gas-liquid chroma tog raphy. The petroleum additives had no signifi-cant effect 

on the CBE composition. The possibility of microconcentrations of 

hydrocarbons forming in intrusive rocks was not excluded; however, this is a 

problem that can only be solved by superdeep drilling under strictly sterile 

conditions.

HYDROGEOLOGICAL OUTLINE

The main hydrogeological investigations conducted on Drillhole SG-3 

focussed on groundwater development conditions and the characteristics of the 

deep layers of the crust - the ancient metamorphic strata and the role of 

water in various geologic processes. In addition to investigations conducted 

on other wells in the Baltic shield, results from geophysical logs, core 

analyses (petrophysical, geochemical, isotopic, etc.), joint system analysis, 

gas-liquid inclusions, thermal ' " data etc., were also used in 

interpretation.' Hydrogeological and helium surveys were also conducted along 

major fault lines.

GROUND WATER OF THE PECHENGA

Drillhole SG-3 penetrated a section of the subartesian basin corresponding 

to ancient Proterozoic secondary artesian basins, structurally related to 

intermontane basins. The section is separable into two stages? the upper is 

composed of metamorphosed sediments and volcanogenic formations of the 

Pechenga complex, and underlying are intensively metamorphosed Archean rocks 

(artesian basin basement) The average porosity is less than 1%, with a 

maximum of 2-3%; therefore, the spatial distribution of fluids is governed by 

fracturing of the water-bearing rocks. A zone of exogenic jointing ranges in 

depth, but averages 800 m. Ground water is only slightly mineralized, being 

derived from atmospheric precipitation. Due to very weak exogenic fracturing,

111
2 transmissivities rarely exceed 1-2 m /day, and are greater only in areas of

tectonic disturbances. Multidirectional fractures were discovered at depths 

of 2.5 - 3 km. From 2.5 to 4.3 km their direction is predominately vertical, 

but the deeper fractures are widely spaced and oriented horizontally. Below 

8.2 km the fractures are again more vertical.

The zones of increased jointing are nonuniform in depth and their 

thickness ranges greatly. Down to depths of 4.5 - 4.6 km fracture zone 

thicknesses ranges from 20 to 80 m and are rather sparsely distributed

500-1500m. The rocks outside these zones are nearly impermeable

. Q -5_ -6 millidarcys). The intervals of increased jointing fall into large

r zones 500-800 m thick, and enclose 2 or 3 of the local observed maxima. These 

zones comprise the fracture-vein systems depicted in Figure 1.77. The permeabi

lity of these zones is comparably small, and formation pressures are low. Three 

such zones are identified down to 4.5 km; and below this depth individual fract

ure zone thicknesses increase but their spacing reduces.

The lower part of the section has been named a zone of regional tectonic 

schistosic development, or more appropriately a zone of regional 

disaggregation. Its base is at 9 km, and the total thickness exceeds 4 km. 

The entire zone contains free or gravitational water. A constant inflow of 

water was observed during drilling. Drillhole testing yielded hydraulic 

conductivities of 10 m/day at 6170 - 6470 m.

GROUND WATER CHEMICAL COMPOSITION

Ground water circulating in the regional fracture zone (exogenic) is of a 

calcium bicarbonate composition with salinities rarely exceeding 0.5 g/1/ The 

nitrogen and oxygen composition indicates a meteoric origin for these waters.

Ground water in the interval 0.8-5 km is of sodium-chloride composition, 

slightly alkaline, and salinities increase with depth reaching saturation in 

some intervals; salinities reach 24 g/1 at 900 m, and 51 g.l at 1200-1350 m. 

In the basal portion there is a relative decrease 'in sodium, and the water is 

characterized as predominately the chloride sodium type (little change); 

however, salinities were significantly higher.

Ground water in the zone of regional disaggregation (4.5-9 km) is not 

hydraulically connected with the overlying zone; the water instantaneously 

rose 80 m when this zone was penetrated. Water from 5.3 to 7 km is neutral 

and slightly alkaline, with a sodium chloride composition. Below 7 km

12
£S-2 "^/j£

Figure 1.77. General hydrogeological cross-section of Drillhole 

SG-3 test area:

1 - zones of negative temperature anomalies; 2 - zones of 

intensive fracturing; 3 - zones of highly mineralized water; 

4 - fracture-vein and fracture reservoir systems; 5 - zone of 

intensive micromovements; 6 - boundary between the III and IV 

volcanogenic-sedimentary cover; 7 - temperature, °C; 8 - wells.

113
the situation changed abruptly/ water became highly mineralized (saline), was 

neutral or slightly acidic, and the composition changed to a calcium and 

sodium-calcium chloride type. The lack of complete analyses of the brine 

inflow below 8 km made it difficult to identify brine components.

The gas from 0.8 to 2.5 km had significant concentrations of hydrocarbon 

gases. The hydrogen content increases with depth and predominates from 2.8 to

3 km. Helium content also increases with depth, and at 6 km it is 

commensurate with hydrogen. The inertness of the helium makes it the best 

indicator of fluid inflow into the drillhole. Gas analyses of the drilling 

mud and the gas composition in the intercrystalline pores and fluid inclusions 

suggest that at 5.5 - 6 km, dissolved carbon dioxide gas begins to be 

significant; however, gas saturation of ground water, on the whole, is rather 

low.

GROUND WATER AND HYDROPHYSICAL ZONALITY

Gravitational water is distributed throughout the entire thickness of 

metamorphosed rocks (more than 10 km), marking the first time that ground 

water was found under such conditions. Based on chemical composition, the 

water for much of the section was similar to deep metamorphosed marine 

sedimentary water of the ancient platforms (including the Eastern European), 

piedmont, and intermontane basins, indicating that the water preserved in the 

sedimentary rocks was syngenetic with- the primary deposits, but underwent a 

long and complex evolutionary process.

Table I.33-presents the results of isotopic analyses of carbon dioxide and 

hydrogen in core samples to study the origin of ground water in the 

metamorphosed rocks. Some depletion in carbon dioxide and the enrichment of

deuterium may be due to the fact that a significant part of the water was i

consumed early in the process^f metamorphism in the formation of other 

hydroxyl-bearing minerals.' These waters were most probably initially 

sedimentary, but then underwent a long and complex evolution.

Several hydrogeologic zones are identified in Table 1.34: 1) zone of 

regional ground water flow (zone of exogenic disaggregation); 2) upper zone of 

fracture water development (zone of metaraorphic compaction); 3) zone of 

regional tectonic schistosic development and hydraulic disaggregation of the 

rock; and 4) a lower zone of fracture water (lowest zone of disaggregation).

During progressive metamorphism, water is released from the hydrated 

minerals (chlorites, epidote, mica, etc.). Chemical bonding of the water is

114
O cr

fv ^

vP

 0°

3 p^

>

cr

c

{/> 

(P

O

F
9TT

1 I'

r

r

r 

e'

e' 

s'

0' 

0'

6'

r

0'

f

£l

0'

s

0'

£1

If

r

V"

:

3

I

1

I

I

I

1

r

f'

fc

s'ei

o's

C'Q

o's

c s 

'8

O'l

e's

o'te

t'l

9'S

e'i

'OS I 

r.

s

,'

l'S6

s'se

8*;%

'66 9 

16 I 

Tee

S'06

s'se

O'OOl

l'E6

o'ie

9'08

O'OOl 

6'06

9'I6

i*

_p

H

t

yy u 

,'e

9'S

MM

ne

a

o'iy

E-«

S'68

"

t*.

s

S'S

S'S

t'o

HpO

t 6 

8'0

*

 HpO

e'o

 HpO

il s

n

3

t'S

S'S

e'o

HpO

c y 

e'o

e'o 

s'o

 HpO

O'l

S'O

 1190

I'l

 HpO

£s

o

a

S'S

re

"ft

y t 

t'i

6'0 

'I

""It

S'l

 HQO

S'l

 Hyo

**

r.

e's

t'e

n

I t 

S'S

's

l'-S

 HpO

?.

 HpO

o's

o y 

SM

n

o y 

Hfc 3

o

s

S'E

O'E6'S

I't

c y 

o't

S'E

S'S

o's

c s 

i> 0 

9'S

e's

S'E

I t S'E

E'E

I t 

E't

S C 

n

I't

9't

6'S

c y 

I'S

o's

9 S 

t I 

i'S

s'e

S'O

rt

S 8 O't

6'S

i y 

e's

s t 

r.

E'O

S'S

t'9

9'6

O'E

y b 

e'9

6*9

t'S

E'S

y y 

0*9

9'e

e's

e't

t'S

o's

i i 

e's

s t 

n

9'0

rs

S'9

6'0l

e's

6'8

e'si

O'Sl

C'll

t'y

i y 

'6

s'e

0'9

'8

t'e

S'9

I 8 

9'ei

t y 

n

t

0 b 

O'S

O'i

S'll

SI S 

3'0l

S'll

S'll

S'S

y i 

e'e

s't

6'8

b I 9'8

e'i

S I 

I S'O 

y y 

n

I I 

1'9

t'i

i'Sl 

9'9

11 8 

S'll

O'S!

t'ei

u s 

e e 

11 0 

t'O!

I'e

S'l

y y o's

e'i

i j 

O'Ol

c c 

n

i y 

S'9

S'l

S'9

8 I 

I'Sl

6'S 

S'S

I i 

8 0 

b 

O'Ol

O't

t'S

y t O'l

9'S

<» c 

S'i

s s 

r.

6 I 

S'S

t'S

1'9

t y 

i'6

O'l 

O'S

Q I" 

s'y

9 L 

s'e

i't

e'e

t'y 

i't

I'S

f 0 

n

a

S I 

e't

S'S

e'9

6'E

9 I 

re

9't

s't

i y 

y i 

S 0 

I'Ol

e't

i'i

i'e

S'E

S'S

S I 

S'9

y y 

r.

I'S

S'E

S'E

S'S 

S'S

S'E

i'E

s'e

y i 

i y 

y y 

e'e

i'S

S'9

I'S 

'6I 

t'Sl

0 I 

I'l

9 9 

' » 
1

o

3

S"f 4

5

G

fMi,

6'

o6nnuo> ¥

24199

24265

26681

26686

26688

26721

26722

27282

27284^1'£>

28748

28767a

287 8a

34569

31570

37804

;

 Jt>-^r>j- t. GJ

7d*f> /HOJ

7932

8028

~~^8360

8862

10182 10 ICO

10182 10 190

V^oCJC

rHcuc

BHOTHTOBUiL»te«C

( TeHeasr^MHTM a 

rfirbi) 6fo4ite. #ri«i< / j i i* , \

"^ 'y '

TajlbK-<SnOTHTTpeJCOJUITOBfalH aHeu lr °

Tr«w.c)/tie p r)t?/^S

^ B.ioTHT-aM$H<5o;inviantOK.iaaoBue

c.iaHUbf

 * . .*

^^n^KitO//^.

/ HaycjJwajiHbje

k MC.iaHOKpaTOBbie 

' rHCHCbl

MyCKOBHT H3

TMeiica /*iu^£cvf*c.

«*^i

£D «'«

/W

 78

s

 82

* "

 80

92

 82

 78

**>- 

+ 10,6

+ 10,4

+8,8

+ 10

+6,9

+ 11,8

+ 9,4

 ***»

.0...

 40

 50

 40

 60

 35

 30

m.

-^-o,u ' fl n

-8,0

+7,0

+8,0

~6

-i-9

 6,4*

r*HV3TTv^

C^^3 fJQtt^X

HSJT^

To )Ke

MarMa- ,

THMCnpopa6OT3HHblH

MOpCKOU

BOJOH

HUH

Mjr*i<a 

THMCCK1IH

1| vj It njatit

_.

cio

f reuwv^

Scdj^A^lsyi^

I-'33

117
00, 5kwii!<rS

Average chemical composition of Archean paleogneisses and 

enderbites comprising the basement of the eastern portion of 

East European Platform and the calculated composition of the 

continental crust (% of dry matter)

OiuicW

SiO,

TiO2

AI 20,

Fc20,

PeO

MnO

M KO

CaO

Na^O

KjO

Mnc/i£«-rfpo6

Honf[/& 

pajpe3e, %

^

EajmtAcKiiA

1

65,05

O.G8

16,55

1,03

6,17

0,07

2,33

1,88

3,11

3,05 

0,08

69

18,7

2

08,18

0,32

16,86

0,64

2,17

0,03

1,41

2,54

5,40

2,38 

0,07

92

46,2

rp»HMTO.rneAco«uA cjioft (iftWtite-grtdjSS

tUIIT

3

67,27

0,43

16,77

0,75

3,33

0,04

1,68

2,35

4,73

2,58 

0,07

161

64,9

i&/$

4

65,27

0,60

17,19

1,39

5,63

0,08

1,99

2,75

2,91

2.07 

0,07

25

47,4

k -» A/W<i'<'Vi< 

\£> tl^nitvVL

5

68,34

0,55

14,37

1,05

4,87

0,07

1,57

3,59

3,08

2,33 

0,18

25

39,1

6

66,68

0,59

15,91

1,21

5,28

0,07

1,79

3,12

3,02

2,18 

0,12

50

H6.5

-rCpCAIICC

Tno CAGIO

7

66,91

0,52

10,28

1,03

4,44

0,01

1,74

2,79

3,75

2,35 

0,10

211

100

C l_d#rr rpauy^MTo-nieAcoBuA c»oH &,r&«v\t\r 

)'. <?:< -^-"J

ix i i DajlTHOCKlin tUHT

8

71.29

0.29

15,55

0,83

1,59

0.03

0.83

3.39

5.18

0,92 

0.11

6

H« OIH).

Uyki£^

9

65.49

0,54

16,47

1,43

3,90

0,10

1,87

4,59

3,92

1,69

14

He-en p.

Up\O£4->.

10

67,23

0.46

16,19

1,25

3,21

0.08

1,56

4.23

4,30

1,46

0,11-

20

H«--onp.

Ortcife/l*

^j^^cc^aig^^

II

66,16

0,58

15,30

1,94

4,60

0,06

2,10

4,91

3,19

1,05 

0.16

13

82,0

70..54

0,30

15,78

0.72

1.60

0.03

1,76

2,98

4,55

1.74 

He-^enp.

6

12,3

13

65,18

0.56

16.94

1,40

3.33

0.08

1,91

4.65

4,45

1,50.

\.ii\i

H«-OTIp.

v/nd*'-!-.

41

50,4

oo 1-3 - biotite plagiogneisses of the Kola Series from the Kola

Drillhole SG-3 section (1 - meso - and melenocratic,

2 - leucocrratic, 3 - weighted average composition) , 4-6 - rock

of the Cheremshan Series from Minnibaev Well 20.000 section

(4 - garnet-sillimanite-biotite crystallized schists, includin

the high alumina schists, 5 - hypersthene plagiogneiss,

6 - plagioclase weighted average average composition),

7 - average composition of the plagiogneisses of the granitegneiss layer, 8 - enderbites of the Kanent'yav massif, Kola 

peninsula [20], 9 - enderbites of the Volnavvol complex, Karel

[76], 10 - average enderbite composition of the Baltic Sheet, 

11 - enderbite-gneiss of the Prikazan Series (Nurlyat complex) 

from the Ul'yanov Well 2000 section, 12-14, Plagiogneiss of th

Iks Series from the Tuymazin well 2000 section (12 - biotitic, 

13 - hypersthenic, 14 - weighted average composition), 

15 - average composition of the enderbite-plagiogneiss complex

of the granulite-gneiss layer, 16 - calculated composition of 

protocrust.
associated with the relatively low-hydrated minerals (epidote/ micas, etc.). 

Evolution of the highly hydrated minerals in the main stage of metamorphism 

led to the generation of solvents and an increase in the volume of 

gravitational water/ which together with primary sedimentary water, is not 

uniformly distributed within the pore spaces and the system of microfractures 

along grain boundaries.

Remobilization of the water in the metamorphosed strata controls the 

processes leading to disaggregation of the rocks and an increase in void 

volume. First, high pore pressures are responsible for the microfractures at 

points where the volume of regenerated water is greatest. Second, this water 

impedes complete compaction during recrystallization, since the release of 

water from the rocks is difficult due to the low permeability. Third, the 

raetamorphic water is highly aggressive and is able to dissolve certain rock

components, increasing their overall void volume.

_Y Hydrogeologic studies indicate extremely low permeabilities (10 . m/day)

in the lower part of the third zone, but it is nevertheless significant since 

up to now it has been assumed that metamorphic rocks at such depths are 

impermeable. Because of the extremely low permeability and the great number 

of isolated voids (microfractures) water has been preserved in the zone of 

desaggregation for more than one billion years. Thus, analyses of the 

distribution of water-bearing zones and the nature of the fracture systems led 

to the conclusion that the source of the fluid in the zone below 4.5 km was 

mineral dehydration during metamorphic transformation.

Calculations showed that in the interval 4-6.8 km, total water losses

7 2 comprised 5.5 x 10 g/m , or 6.7% of the original rock volume. Analyses

based on average mineral composition show that the total volume of the

minerals in the transition from the green^schist to epidote-amphibole facies «_< >

comprised 0.96 of the original volume, which combined with the released water 

is 1.027, or 2.7% greater'than the initial volume. To preserve this initial 

rock volume, water would have to be compressed by 1.7 times requiring 

pressures of some 30 gPa, corresponding to pressures at mantle depths (90-100 

km). An increase in volume can only occur through fracture continuity, since 

rock tensile strengths are an order of magnitude less than the pressures 

developing during the release of water. Figure 1.79 shows the strong mineral 

crystal deformation and void development (fracture continuity) from the 

extremely high hydraulic pressures. Mineral dehydration could not occur

otherwise.

119
Figure 1.79. Talc-biotite-tremolite schist (8028 m) . 

Section, X600. The intercrystalline microfracnures are quite 

evident.

120
Fracture orientation is governed by the spatial orientation of the strain 

ellipsoid at the time of formation. In a relatively quiet tectonic setting 

near vertical fractures are formed. If the horizontal stress significantly 

exceeds the lithostatic load, a known characteristic of the Baltic shield, 

then fractures may have a horizontal orientation that may open up over time. 

The regional schistosic development seen in the section of SG-3 is related to 

this process; the orientation of the schist development is subhorizontal and 

is independent of stratigraphic boundaries. Inasmuch as high horizontal 

stresses are typical for deep crustal zones, this phenomenon of regional 

schistosic development may be detected rather often. Based on the ratio of 

free and bound water at various stages of metamorphism, hydrogenic 

disaggregation may likely occur in rocks of epidote-amphibolite and 

amphibolite facies.

The nearly coincident boundaries of the geochemical zones with the 

boundaries of the stratigraphic subdivisions and their restriction to definite 

types of metamorphism suggests that the essential influences on ground water 

formation is the initial habit of the rocks, the degree of their metamorphic 

transformation, and contemporaneous metamorphic trends.

The hydrodynamic zones differ from one another not only in their 

qualitative and quantitative characteristics of fracturing and in transmissive 

properties and hydrostatic pressures, but also in a range of changes peculiar 

to each zone in lithostatic pressure, temperature, and gas and chemical 

composition.

The main mass of ground water was the product of an exogenic water 

exchange in the zone of regional ground water flow, whereas clearly the water 

in the lower zones bears an endogenic nature. The total quantity of

chemically bound water and the nature of its bonds (highly hydrated in the two /

upper zones, and a lower hy. drat ion in the lower) permits the hydrogeological 

evolution of the rock masses to be reconstructed. The model of hydrophysical 

zonality presented in Table 1.34, not only explains the nature of the 

hydrothermal fluids unrelated to intrusions, and allows us to understand the 

mechanism of regional schistosic development in the zones of disaggregation 

and the formation of certain types of tectonic disturbances, but also 

fundamentally changes our perceptions regarding the circulation of ground 

water in the crust.

121
EVOLUTION OF THE CONTINENTAL CRUST IN THE PRECAMBRIAN 

Data from the Kola drillhole opened up the possibility to address the 

problems of Precarabrian crustal evolution from the standpoint of a 

3-diraensional model where the addition of a known third dimension gives rise 

to the possibility of reconstructing the geologic process that operated in the 

past, and evaluating alternative hypotheses regarding the structure and 

development of the deep crustal zones composed of metamorphosed Precambrian 

rocks.

GEOLOGIC MODELS OF THE PECHENGA REGION

The three-dimensional model of the Pechenga structure shown in Figure 1.80 

(in pocket) was based on drillhole data/ gravity-seismic surveys, and wells 

located in line with SG-3. Based on these data a number of conclusions were

drawn regarding the structure of the Pechenga complex. The structure

U

comprises a graben-syncline, bonded on the south by a zone of regional faults

A 

with depths greater than 20 km. Gravity surveys yielded a decreasing gravity

gradient that repudiated the previously held notion of an overturned north 

limb, and suggest that the southern regional fault zone is composed of 

parallel-contiguous reverse faults. The base of the fault zone is "sealed" by 

a hypabyssal andesitic intrusion. The maximum thickness of the 

volcanogenic-sedimentary formations of the complex was established in the 

central part of the graben-syncline/ in the vicinity of the Por'itash fault, 

as being greater than 8 km. Despite the interpretations of surface 

gravimetric and seismic survey data, the drillhole penetrated a thick 

granite-gneiss rock mass at 6.8 - 11.6 km, containing many amphibolite bodies 

comparable to the Kola Series. Geologic and geophysical data also indicated 

that the Conrad layer could not be explained by either a transformation from 

more silicic to basic rocks 7 ,9r by an abrupt metamorphic boundary, or by 

subhorizontal tectonic zones.

HISTORY OF THE GEOLOGICAL DEVELOPMENT OF THE PECHENGA REGION 

Drillhole SG-3 data have contributed profoundly to our understanding of 

the historical continental crustal development of the Pechenga region. 

Development has been subdivided into two great cycles: the Archean (greater / 

than 2.6 by) which includes two stages; 1) sedimentation and volcanism, and 

2) folding, metamorphism, and ultrametamorphism; and the Proterozoic (2.6 - 

1.1 by) (second cycle), which includes 4 stages of development; 1) subsidence

122
Figure 1.81. Reconstruction of the proto rock composition of the 

Archean complex from Drillhole SG-3 (odd) and the surrounding 

surface (even).

1 - trend of magmatic differentiation; 2 - trend of sedimentary 

differentiation; 3, 4 - amphibolite; 5, 6 - hornblende-biotite 

paleogneiss; 7, 8 - biotite-plagioclase gneiss; 9, 10 - biotiteplagioclase gneiss with VGM; 11-16 - average composition 

(11, 12 - rocks of amphibolite group; 13, 14 - rocks of 

plagioclase group; 15, 16 - rocks of Archean complex).

123
of the midcontinental mobile belt, 2) andesite-basalt volcanismr 3) 

picrite-basalt volcanism, and 4) a stage of plicative-rupture dislocation and 

metamorphism. The structural-metamorphic evolution was consumated by a 

platform activization stage.

The Archean metamorphic complex (6842-11,622 m) penetrated by Drillhole 

SG-3, is of mixed composition and has a rhythmic-stratified structure. The 

preservation of deep rock sections, nearly unchanged by migmatization and 

metasomatism of the metamorphic rocks, permitted the original compositions to 

be reconstructed using the petrochemical diagram of Fig. 1.81. Using the 

composition and content of rare earth elements the amphibolites are identified 

with the volcano-plutonic association of Archean basic rocks of the green 

schist belts (Figure 1.82).

The first Archean stage is characterized by an accumulation of thick 

sedimentary strata (argillaceous-siliceous) and active volcanism associated 

with an outpouring of rhyolitic, dacite, and andesitic lavas with minor 

basalts and ultramafic rocks (basaltic-andesitic formations).

The tectonic structure of the second Archean stage, based on analogous 

Archean complexes present on the surface, represents a synclinoria zone or an 

asymmetric-syncline in combination with a dome-shaped structure. Surface 

observations point to a recurrence of plicative and fracture deformation of 

the Kola Series from metamorphism and ultrametamorphism; however, Drillhole 

SG-3 cores failed to distinguish these different-aged tectonic elements. The 

time of metamorphism for .this stage was 2754 + 40 my. Age dating and the 

products of earliest granitoid magmatism indicate . there was a single zonal 

series of progressive metamorphism and ultrametamorphism of the Kola complex. 

The Archean cycle culminated with consolidation of the subcrystalline 

formations (cratonization) and deep faulting.

The Proterozoic cycles are characterized by the formation on the Archean 

basement of the midcontinental mobile Pechenga-Varzu belt which trends 

southwest along the entire Kola Peninsula from Norway to the White Sea. Four 

stages are identified in belt development: 1) subsidence of the belt, 2) 

andesite-basalt volcanism, - 3') picrite-basalt volcanism, and 4) 

plicative-rupture dislocation and metamorphism.

The first stage was distinctly established on the surface by the 

development of the Tundra Series in portions of the southern edge of the belt, 

but radioactive dating could not precisely date the discontinuity between 

consolidation of the Kola complex and the onset of subsidence. The
\/o

Figure 1.82. Trends in_the distribution of La and Yb in rocks of 

the Archean complex from Drillhole SG-3 and their identification 

with the main structural-genetic series of the Precambrian and 

the Phanerozoic: (ct*nv*-*

125
I - melanocratic plagiogneiss with VGM; 2 - mesocratic two-mica 

plagioclase with VGM; 3 - leucociratic two-mica plagioclase with 

VGM; 4 - biotite plagioclase (K^>10%); 5 - biotite plagioclase 

<10%); 6 - biotite gneiss; 7 - leucocratic epidote-biotite 

plagiogneiss; 8 - mesocratic epidote-biotite plagioclase; 9 - 

hornblende-biotite schist; 10 - hornblende-biotite-plagiogneiss;

II - Fc.-TA-amphibolite; 12 - Fe-amphibolite; 13 - AZ-Mf

-amphibolite; 14 - Si-amphibolite; 15 - gabbro-amphibolite; 16 - 

talc-actinolite schist; 17 - postfolded porphyry granite; 18 - 

average (a) and limited (b) concentration; 19 - granitoid, 

Litsko-Aragub complex (PR^)/ after [18]; 20 - trend of 

metaextrusive and metaintrusive rocks of the Pechanga Complex (a

- metabasalts, b - metaandesite-basalts of the rift-continental 

stage, c - metagabbro-diabases, d - metabasalts of the riftoceanic stage); 21-25 - trends (21 - sedimentary differentiationsand-clay of the Phanerozoic and metapsammite-metapelites PR^> 

after [3], 22 - gabbro-plagiogneiss series of the Early Archean, 

after [108]; 23 - primary-crustal granitoids of Early Archean 

Kola Peninsula, after [101]; 24 - intrusive rocks; 25 - extrusive 

rocks, Early Archean greenstone belts and extrusive series of the 

Phanerozoic).

126
paleotectonic conditions during subsidence can only be generally 

characterized, inasmuch as the rocks of the Tundra Series underwent intensive 

regional schistosic development and zonal metamorphism, ranging from a 

sericite-chlorite zone in the greenschist facies to a sillimanite-muscovite 

zone in the ."!_ ." __ amphibolite facies. ...

The transition from the first to second stage was marked by intensive 

volcanism under subplatform conditions suggested by the great thicknesses of 

lava flows, but also by an exceptional uniformity in dip and areal extent of 

the thin cover of sedimentary rocks. Petrologic and geochemical data show 

that volcanism began with an outpouring of uniform undifferentiated magmas, 

whose later evolution and differentiation resulted in an outpouring of 

trachy '-salts (Figure 1.84). The mechanism is determined as syntexis, where 

basic chamber magma is introduced to the "cool" silicic crust accompanied by 

melting and assimulation of crustal material and, consequently, mo^ifl co-fron <sf 

the original composition. The subsequent differention of the melt resulted in 

the separation ou;t of andesite.

Between the second and third stages a discontinuity is not so distinct; 

however, its presence is demonstrated by the development of weathering on the 

top of the Pittiyarvin Formation/ an abundance of magnetite fragments in the 

Luchlompol sandstones, and a distinct succession of volcanics. Hence, the 

onset of the third stage was sharply marked by an outpouring of 

undifferentiated tholeiitic magma, forming a rhythmic tholeiite-basalt 

formation, with an apparent thickness of 1.9 km.

Specifics of the third stage are reflected in the nature of formation of 

the sedimentary deposits. Thus the Zhdanov Formation has two large distinct 

sedimentary cycles, as expressed in Fig. 1.83. The facies and salt 

composition of the ground water is indicative of primarily sedimentation

4

conditions.

A detailed reconstruction of the entire succession of tectonic events is 

impossible; nevertheless, the data permit a new interpretation of the regional 

structure. Deformation and metamorphism of the Pechenga Complex is related 

not .t.o ' the final stage of Middle Proterozoic geosyncline development, but 

v/fi> the protoactivization of Early Precambrian Kola Peninsula structure. The 

regular variation with depth in structure and texture of metamorphic rocks, 

the definite orientation in these rocks of quartz, carbonates, mica, and 

amphibole is evidence that under thrust movement took place along with 

progressive metamorphism of.the Pechenga Complex.

127
S«0 2 JO W SO

r-n/ r^fraj^^FvT^fh-H*r-- 7K?SU \z--\9

Figure 1.83. Lithologic-petro chemical characteristics of the 

metasedimentary rocks of the Pechenga complex.

Formations: a - Televin, b - Kuvemerin, c - Luchlompol', 

d - Zhdanov. Rocks: 1 - metaultrabasites, 2 - metagabbrodiabases, 3 - dolomites and limestones, 4 - dolomitic and 

calcareous metasandstones, 5 - metasandstones and metasiltstonessandstones, 6 - metasiltstone-sandstones and metapelites, 

7 - admixture of carbonaceous material, 8 - metatuffs and 

metaphyllites, 9 - carbonaceous matter, 10 - sulfates. Rock 

composition from Drillhole SG-3 (a) and regional surface rocks 

(b): 11 -'sandstone-dolomite and limestones, 12 - dolomitic and 

calcareous metasandstone, 13 - calcareous metasandstones, 

14 - metasandstones, 15 - metasiltstone, 16 - metapelites, 

17 - metatuffites, 18 - trends of sedimentary differentiation 

(I - sandstone-dolomites and limestones, II - dolomites and 

calcareous sandstones, III - calcareous sandstones, 

IV - sandstones, V - siltstones and silty pelites.

128
MiMai
5£7

10 SO 70

4 4

444

4 4

444

4 4

444

^rix

4 4 <

4 4 4 

4<4V

sra^

4 4 4

S717*

>fl?<7,

>"ff»

VTTff,

SS2J*

30 MgO

90

Figure 1.84. Geologic-petrochemical characteristics of 

metavolcanic rocks of the Pechenga complex.

Formations: a - Mayrvi'nsk, b - Pirttiyarvin, c - Zapolyarnin

d - Matertin Principal types of rocks in geologic sections?'

} " ^E10^?3 ' ? ' Mtapicrite-basalts, 3 - metabasalts,

4 - metatrachybasalts, 5 - metaandesite-basalts

6 - t metatrachyandesite-basalts, 7 - metaandesitis, 8 - metatuffs

basic (a) and average (b) composition, 9 - metatuffites, a tt5 '

i0 ~l^g f aSaItS ' ll " sPilitization . Metaextrusive rock

composition (a - average and b - particle values),

12 - metapicrite, 13 - metapicrite-basalts, 14 - olivine

metabasalts, 15 - differentiated meta basalts, 16 - metabasalts

17 - (missing) is - low alkaline metabasalts, 19 - spilites

20 - metatrachybasalts, 21 - metaandesite-basalts,

22 - pyroxene-divine metaandesite-basalts, 23 - (missing)

; * - metaandesite. Trends metaextrusive rock differentiation, i

25 - in lower and 26 - in upper parts of volcanogenic

Overthrust movement is associated with a sharp transition from isotropic

to anisotropic metamorphic rocks with respect to elastic properties and an

c 

interval structure in the zones of regional shistosic development, manifested

A

by a seismic boundary. Outpouring of extrusives was accompanied by low 

temperature autometasomatic and metamorphic alterations with the formation of 

hydroxyl-bearing minerals. Progressive metamorphism of the entire complex 

increased temperatures up to 500-600°C, increasing the pressure and inducing 

an autoclave effect with the release of synmetamorphic fluids, enriched in 

chlorine, iodine, barium, strontium, and potassium. This effect resulted in 

rock deformation and the manifestation of hydraulic disaggregation.

The Luchompol fault was definitely active over a long period of time. The 

dacite metaporphyri.tes in the SG-3 section correlate in age and composition 

with the volcanic-plutonic complex of the southern part of the Pechenga 

structure (Por'itash fault), and the extrusives formed in the southern 

basalt-andesite formation are orogenic, yielding the assumption that at depth 

the Luchompol' fault is connected with the steeply dipping Por'itash tectonic 

zone, and that this discontinuous dislocation created a disjunctive 

reverse-over thrust body in the Pechenga structure. It is pointed out, 

that in the Luchompol' fault and immediate vicinity, the regional schistosic 

and the metamorphosed sedimentary and volcanic rocks contain anomalously high 

concentrations of argon and helium, evidently introduced by the fluids.

EVOLUTION AND VERTICAL ZONALITY IN MINERALIZATION 

Core studies from SG-3 yielded data on the vertical zonality in 

mineralization in the deep zones of the crust for the first time and 

established that this zonality was developed in stages. This single section

shows all the mineralization processes, related to sedimentation, volcanism,

/ 

intrusive magmatism, and hydrothermal activity.

Evidence in the Drillhole SG-3 elicits the assumption that the formation' 

of copper-nickel ore deposits in the Pechenga complex was connected with the 

protoactivization of Early Precambrian crustal structures. The process 

reached its maximum in the Middle Proterozoic when stabilized continental 

crustal blocks were broken by large faults.

Based on the data from Drillhole SG-3 it can be assumed that metamorphism 

took place under a geothermal gradient of 50°- 70° /km. Ultrabasites and 

copper-nickel ores were metamorphosed under greenschist facies conditions (T = 

350 - 450°C, P = 0.2 - 0.3 gPa).

132
The types of ore mineralization exposed in SG-3 agree well with the 

Archean and Early Proterozoic history in the Pechenga region. The Kola Series 

comprises intensively metamorphosed ferruginous quartzites, iron-titanium ores, 

copper-nickel mineralization; and the Pechenga Complex includes less 

metamorphosed pyrite mineralization and copper-nickel deposits. However, this 

structural scheme clearly compliates the development of low-temperature 

hydrothermal mineralization which was encountered for the first time in the 

lower parts of the Pechenga Complex, and subsequently down to 11 km. Although 

the scale is small, it nonetheless modifies one's notion of the formation of

ore-bearing fractured structures. The great stability of the mineral 

associations in the zones of regressive dislocation metamorphism, low 

temperature formation of sulfides, and the results of isotopic analyses of 

sulfur indicate a subcrustal origin for the juvenile hydrotherral fluids.

EVOLUTION OF THE EARTH'S CRUST IN THE PRECAMBRIAN

A description of the deep structure and chemical composition of the 

Precambrian continental crust is one of the fundamental problems of 

contemporary geology. Any sound solution to this problem should be able to 

specify the primary evolution in the composition of the ancient complexes from 

the protocrust to the present continental crust, identify the developmental 

mechanism, establish the specific fluid regime and P-T conditions for 

metamorphism in the Archean and Proterozoic, and as a consequence, determine 

the origins and trends of ore-forming systems.

The fundamental basis for assuming the basaltic composition of the 

protocrust in the past has been Geoffrey's two-layer model; however, recent 

interpretations based on deep seismic soundings of the Canadian and Anabar 

shields, the Eastern European platform and others, disputes the two-layer 

model since the Conrad surface, the surface that separates the "granite" from 

the "basaltic" layer, is not present everywhere under the continents.

The Conrad surface was also not detected in the section of Drillhole SG-3, 

and further seismic data- shows that where the "granite" layer is expected, 

basic metamorphic rocks occur; and conversely, where the "basaltic" layer 

should be expected, a migmatite-plagiogneiss complex occurs, which to date 

extends down to 11.6 km.

Data from SG-3 and other deep drillholes into the crystalline basement 

rocks of the Eastern European Russian platform have for the first time 

established a factual basis for addressing these problems. A seismic model,
based on these data of the ancient platform crust and the results of studies 

in the Eastern European Russian platform are presented in Fig. 1-85.

Comparisons of SG-3 and other deep drillholes into the basement rocks of 

the Eastern European Platform elicited a single geologic-geochemical scheme 

for the structure of the continental crust comprising three layers: 

granite-gneiss (0-15 km), granulite-gneiss (15-30 km), and a very deep layer

(protocrust) (30-40 km). The extrapolation of geochemical trends down to a 

depth of 35 km suggests that the protocrust was formed from rocks close to 

sodic dacite in composition.

134
Figure 1.85. Seismic model of the ancient platform crust

(a),^after [77], and hypothetical (b) and studied (e) deep

sections of the Eastern European Platform: 1 - volcanic and

volcanogenic-sedimentary metamor^hic rocks, 2 - granites,

3 - metaultrabisic and talc-acti^nolite schists, 4 - amphibolites

and two-pyroxene basic crystalline schists, 5 - biotite

plagioclase schists, 6 - plagiogneiss and enderbites,

7 - biotite-amphibole plagiogneiss and hypersthene dioritegneiss.

135
Figure 1.86. Variation in chemical composition of the enderbiteplagiogneiss complexes in a section of continental crust:

1 - average composition of metamorphosed complex, 2 - average

composition of the granite - and granulite-gneiss layers,

3 - extrapolated average composition of the proto-crust

(I - granite gneiss, II - granulite gneiss, III - proto-crust).

136
GEOPHYSICS

Geological-technical conditions of geophysical investigations of the drill 

hole. The diversity of rock types and great length of the hole are important 

factors in the quality of the geophysical data obtained by the in-hole 

measurements. In the interval of occurrence of volcanic-sedimentary rocks 

(2, 005-5,000 m), conditions were favorable for such logs; below this, however, 

particularly in the Archean gneisses and schists, conditions deteriorated. 

The presence of cavities [caverns in the Russian] to depths of 7,000 m 

contributed to the complex configuration of the cross section of the hole.

Geophysical programs for study of the drill hole. Emphasis was placed on 

study of the lithology and composition of the rocks and determination of their 

physical-chemical parameters and stress state. The various missions and , 

corresponding geophysical logging programs are listed in Table II.1.

137
Table II.1

Mission Geophysical Logging program

Subdivision of the section

into members and groups of rocks

Lithologic-composition study

Acoustical (AL), laterolog (LL), 

spectrometric - gamma (SGL), gamma (GL), 

neutron (NNL-T, NNL-N, NGL), impulse 

neutron-neutron (INNL), magnetic (ML).

Detection of zones of 

copper-nickel mineralization

Electrical potential (EPM) and gliding 

contacts (MSC) methods, spectrometric 

neutron-gamma (SNG).

Determination of interval and 

formation velocities of elastic 

waves and attenuation parameters

AL.

Determination of interval and 

formation values of electrical 

characteristics of rocks

Laterolog (LL).

Determination of density rocks Gamma-gamma (GGD-L).

Determination of effective 

atomic number gf rocks

Selective gamma-gamma (SGGL)

Determination of average life 

time of thermal neutrons

INNL

Determination of component geomagnetic field and magnetic 

susceptibility of rocks; attitude 

of magnetic complexes

ML

138
Determination of thermal properties Thermal logging (TL). 

of rocks

Estimation of values of axial, AL, GGD-L, LL. 

radial and tangential stresses in 

rocks; subdivision of the mass into 

zones of different direction; 

detection of fracture zones

Formulation of geophysical, geo- AL, NGL, GL, SGL, ML, LL, GGDL, TL,

thermal, and geochemical models vertical seismic profiling (VSP)/

of the section gas logging (Gas L).

During the first stage of drilling where temperatures were comparatively 

low, and where hydrostatic pressure was low and did not require a heavy 

drilling mud, domestic production-line logging apparatus was used. See figure 

II.1.

The geophysical methods used in the second stage are shown in figure II-2.

Procedure of geophysical investigations. Special procedures had to be used 

for the in-hole measurements.

1. Depth determinations. At a depth of 11 km the variation in the 

length of the cable may be 19-20 m. Marker horizons were determined on the 

logs of each kind, and these-were then used as standards for depth (d),

2. Acoustical log. Measurements have been made to a depth of 11,500 m 

recording longitudinal and transverse waves. The logs are poor for bottomhole 

readings, due probably to drilling mud absorbing the signal. When the hole is 

deepened, the signal for this same interval is better, provided no large 

cavities are present.

3. Gamma log. A Cs-137 standard was used to calibrate to instrument. 

Stability of the apparatus was checked by repeat measurements in an andesite 

porphyry in the 4673-4784 m depth interval.

139
§ -a«

3 $ § s R i

, O.UP...Q.GQ

Figure II. 1. Geophysical methods used in the first stage.

VSP - vertical seismic profiling, AL - acoustical log, AR - apparent 

resistivity, LL - laterolog, MSC - method of sliding contacts, EPM - electrical 

potential method, EML - electromagnetic logging, ML - microlog, TL - thermal 

log, SGL - spectrometric gamma log, GL - gamma log, NGL - neutron-gamma log, 

GGDL - gamma-gamma density log, SGGL - selective gamma-gamma log, INNL - 

impulse neutron-neutron log, NNL-T - neutron-neutron log of thermal neutrons,- 

NNL-S - neutron-neutron log of super-thermal neutrons, Gas L - gas log, 

CL - caliper log, Profile - profile meter, Dipm - dipmeter, Metal 

determination: mag-magnetic, non-mag - nonmagnetic.

140
en

HOq

HOq C

i-h 

O 

 -i

oO*

O 

fD O

oq

- 1 Is I K \* 

|u 1 |S | h h

i : 

i 

i 

i . 

i 

i 

i 

i 

i 

i 

i 

i _________

00 © 0

_LZ]

VSP

AL 

LL 

ML 

TL

SGL 

GL 

NGL

NN

. INNL 

Profil

Dipm

Metal 

Gas lo

OPK
4. Spectrometrie gamma log. This log was made at intervals of 100-500 

m. It measures K-40, RaC 1 , and ThC 1 in the rocks.

5. Gamma-gamma density log. A two-probe modification (15 and 35 cm 

probes) was used to depths of 6,000 m. Below this the column contains 

abundant cavities, and this method was not used.

6. Selective gamma-gamma log. Used to a depth of 3,000 m, this 

technique measures the effective atomic number of rocks in ore zones.

7. Neutron-gamma log. This log was run to a dept of 11,440 m. Cavities 

have a strong effect on the readings; there is a sharp drop in intensity of 

secondary radiation where cavity diameter is greater than 40 cm.

8. Neutron-neutron log. A pair of probes (30-50 and 40-60 cm) were used 

for measurements to 11,510 m to study the lithology of the section.

9. Magnetic log. Vertical and horizontal components of the magnetic 

field and magnetic susceptibility were measured to a depth of 11,500 m.

10. Electrical methods. Various electrical measurements were made to a 

depth of 10,644 m. The method of sliding contacts (MSC) and the electrical 

potential method (EPM) were used in the 0-6,000 m interval. These picked up 

conducting zones including copper-nickel sulfide mineralization. Laterolog 

was used on farther down the hole.

11. Thermal log (TL). Measurements were made while the thermometer was 

being lowered and when being raised in the hole. The scale was at 0.25 and 

0.5°C/cm. Logs were run to a depth of 11,503 m.

12. Vertical seismic profiling (VSP). A continuous log was made to 

11,514 m.
Prospects and Tasks for Improving Geophysical 

Logging of Super-deep Holes

Experience gained in logging to 11,514 m is a basis for predicting

conditions at greater depths both in SD-3 and, other super-deep holes to depths

A

of 15,000 ra. Difficulties in logging are related to the high temperatures and 

pressures. Linear extrapolation of the geothermal gradient (0.019°C/m) gives 

a temperature of 266°C at a depth of 15,000 m in the Kola hole.

The main thrusts of further logging research are:

1. Increasing the capacity to operate at high temperatures and pressures 

and extending the life of the in-hole equipment.

2. Improving "without-cable" information systems - independent 

instruments on the drill stem.

3. Development of multi-strand load-carrying cable.

4. Development of powerful equipment for going in and out of the hole.

5. Development of an optimum system for in- and out-of-hole operations.

6. Development of a system of control of logging parameters.

Density and Permeability-Porosity Properties of Rocks 

Density of the rocks was determined from cores (more than 40,000

measurements), from gamma-gamma density logging, and by in-hole gravimetry. 

Error does not exceed 0.01 g/cm . Permeability and porosity were determine* 

only on cores. Error is not greater than 0.1 percent. See Table II.4.

Acoustical Properties of the Rocks

Acoustical measurements were made on cores as well as by logging. The 

following parameters were measured on cores: velocity of longitudinal waves 

along the axis of the core and perpendicular to this axis; maximum, 

intermediate, and minimum velocity in samples with natural moisture (dry) and 

the same on water-saturated samples; velocity of transverse waves along - the 

axis of the core and perpendicular to this axis; the coefficient K and the

Si

factor A, which are functions of anisotropy of the rock; Youngs Modulus; and 

Poissant's Ratio.

Results of acoustical measurements on cores. More than 30,000 

determinations of longitudinal wave velocity were made and 10,000 of

143
Proterozoic 0-4, SFOO

Proterozoic, 4,500-6/835 m

Archean, 6,835-10,500 m

Amphibolite 2.93

Ultra-metamorphosed

rocks 2.98

144

Table II.4

Rock

Open porosity

Density

Permeability 

mkitL,

Diabase, gabbro, 

pyroxene porphyry 3.0 0.40 0.031

Meta-volcanics 2.90 0.45 0.044

Me ta-diabase, 

meta-andesite 2.89 0.60 0.291

Volcanic-sedimentary

(slates) 2.78 0.55 1.252

Gneisses 2.69 1.19 16,905
transverse wave velocity. For the Proterozoic sediments (to a depth of 6,842 

m), the average longitudinal wave velocity with natural moisture is 5,670 m/s; 

for water-saturated - 6,080 m/s. The average value of longitudinal wave 

velocity for the Archean rocks (6,842 to 11,000 m) is 3,990 m/s.

The idea that velocity for rocks of the same composition increases with 

depth is not confirmed. Maximum values of velocity are found in the upper 

part of the section.

On a basis of elastic properties, the section is divided into three 

parts. The first is to a depth of 4,500 m where the interface corresponds 

generally with the boundary between the greenschist and epidote-amphibolite 

raetamorphic facies. The principal importance of this boundary is that the 

primary composition of rocks below it is preserved. The second interface at a 

depth of 6,842 m is not as pronounced as for other logs. For the main types 

of rocks, there is a great similarity in velocity values obtained by 

acoustical logging and by measurements on cores.

In-Hole Seismic Investigations

Travel time curves were made of first arrivals and phases of P-waves and 

travel time curves of phases of S-waves. Vertical seismic profiling data can 

distinguish strata with thicknesses of 200 to 1,000 m. Average velocity of 

P-waves is 6,500 m/s and of S-waves, 3,600 m/s. Digital methods were used for 

more detailed study of the section.

The wave picture of the Kola hole differs qualitatively and quantitatively 

from that of vertical seismic profiling in platform regions with a thick 

sedimentary cover. Steeply dipping unconformable interfaces and the large 

number of faults contribute to complicated seismic conditions. See Fig. II.6.

Electrical Properties of the 'Rocks

Electrical resistivity was measured in the hole by logging (p) and also on 

core samples (££.). Maximum values were found for diabases, spherulitic lavas, 

and sandstones, and minimum for silstones and phyllites of the Pechenga 

Series. Values of £> and ^^ differ from one another by 1-2 orders. For

example, for meta-diabase and spherulitic basalt at depth of 3,200 to 3,600 m,

4 56 j^ is 6 x 10 ohm-m, whereas £ is 4.5 X 10 to 5.6 x 10 ohm-m.

145
fl

0,2 0,3 i.c

11

H. KM

Figure II.6. Wave field of Kola hole.

The predominate frequencies of P- and S- waves vary little with depth 

and time, indicating low attenuation of waves.

146
MAGNETIC PROPERTIES OF THE ROCKS

The magnetic characteristics reflect the concentration and composition

4 -*

of ferromagnetic minerals, their structural sta>fe and relationship to 

^\

para/magnetic iron-bearing minerals.

The magnetic properties of the rocks of the section of hole SD-3 were 

determined both under natural conditions and on core samples. In the hole, 

the components of the total magnetic field vector H and the magnetic 

susceptibility k were measured. On the core, the following magnetic 

characteristics were studied: magnetic susceptibility k and anisotropy A, ; 

value and direction of natural remanent magnetization J ; the Koenigsberg

factor Q = J /O.S.k; saturation magnetization J , remanent saturation 

n s

magnetization J ; disturbing field H' of reraanent saturation 

magnetization; and the parameter N (see section on "Results of 

magnetic-mineralogic analysis of the rocks") .

These characteristics were determined on an astatic magnetometer MA-21 

and ROKt generator ION-1, thermomagnetometer and vibromagnetometer . The 

procedures of measurement of the magnetic characteristics of the core and 

processing of the data obtained are sufficiently elucidated in the literature,

The results of study of the magnetic properties of the core recovered 

from hole SD-3 are given in table 11.11.

The most representative material on the core (more than 35,000 

determinations) was obtained for magnetic susceptibility, natural remanent 

magnetization and the Koenigsberg ratio.

MAGNETIC SUSCEPTIBILITY

This is one of the most important magnetic characteristics of rocks, 

reflecting their ability to be' magnetized in a constant magnetic field H. The 

differences in k through the section in hole SD-3 were rather considerable.

The results of computer processing of the data on the petrophysical 

intervals showed that 80% of them have a significant difference in k, with a 

probability of 95 to 99.9% (limits on both sides), the latter predominating.

In the Proterozoic Pechenga Complex the maximum average values of k are 

observed in the meta-trachybasalt schists of the Pirttijarvi formation 

(4884-5619 m) 65.10 SI units, and also in the serpentinized peridotites 

of the Zhdanov formation (1541-1678 m) 124. 10~ SI units. Relatively 

high values of k are typical of the talcized and serpentinized picrite
TABLE 11.11 

MAGNETIC CHARACTERISTICS OF THE ROCKS IN THE SECTION OF HOLE SD-3

Type of rock Group of rocks

K-10 5 

SI units Q . Jn -I0 5 , A/m

Proterozoic, depth interval 0-4586 m, zone of sulfide mineralization

Igneous ,

tuffs

Diabases 

Gabbro-diabases 

Ultramaf ics 

Basic tuffs

Mean weighted value

Tuff ogenicsedimentaryTuf fogenic 

Terrigenous , chemogenic

Mean weighted value

88 

105 

6160 

151

561/94*

108 

129

125

3.05 

4.1 

2.23 

1.79

3.13/3.2*

1.94 

7.21

6.05

231 

153 

10,612 

278

1017/218*

50 

825

6.54

Proterozoic, depth interval 4586-5642 m, zone of oxide mineralization

Igneous , 

tuffs

Meta-diabase schists 

Andesite porphyrites 

Ultramaf ics, tuffs

Mean weighted value

Sedimentary Terrigenous , chemogenic

4760 

66 

7067

4542

86

1.2 

4.1 

1.5

1.4

1.02

1,440 

243 

7,639

1,507

88

Proterozoic, depth interval 5642-6842 m, zone of mixed mineralization

Igneous Meta-diabase schists 

andesite porphyrites 

Ultramaf ics

Mean weighted value

43 

56

45

'0.4 

0.2

0.4

23

7

22

Archean, depth interval 6842-10,500 m, zone of mixed mineralization

Gneisses 

Amphibolites 

Ul trametamorphics 

Mean weighted value

20 

70 

'40

46

2.0 

9.1 

1.4

2.5

22 

680 

39

70

*In numerator values calculated for all rocks including ultramafic; 

in demoninator values calculated without ultramafics.
porphyrites of the Materta [Matertinsk] formation/ (19-38).10 SI units/ 

and the andesite-dacite metaperphyrites of the Luchlompol' formation, 5.10 

SI units. The magnetic susceptibility of all these rocks is ferromagnetic. 

The value of k in the metavolcanics of tholeiite-basalt and andesite-basalt 

petrochemical type varies within narrow limits regardless of the extent of 

metamorphism (from 0.5.10 to 1.0.10" SI units) and is

ferroparamagnetic. Minimum values of k are characteristic of the dolomites 

and metapsammites of the Luchlompol' and Kuvernerinjok formations. Thus the 

magnetic anomalies in the Pechenga Complex are related either to the 

ultramafic formations, metamorphosed in greenschist and prehnite-pumpellyite 

facies, or to metavolcanics of alkalic petrochemical type regardless of the 

extent of their metamorphism.

The magnetic susceptibility of the Archean complex in the section of 

hole SD-3 as a whole is lower than in the Proterozoic complex and than the 

Archean rocks which crop out in the drilling area (fig. 11.16). The 

iron-silicate rocks have maximum values of k - (0.6-1.0).10 SI units. The 

ferromagnetic nature of k is also typical of the epidote-biotite-amphibole 

gneisses/ schists and araphibolites/ migmatized by plagio-microcline granites/ 

for which x = (4.6-9.6).10 SI units. These formations as a whole are 

subordinate and tend to be in the lower part of the section (interval 

9541-11/000 m). The background value of magnetic,..susceptibility is determined

by the shadow raigmatites and amphibolites [oebulites -?]. In the shadow

 3 - - 3 

migmatites/ k increases downhole from 0.09.10 to 0.54.10 Si units/ and

in the amphibolites it varies from 0.53.10 to 1.57.10- SI units/ the 

maximum values and greatest spread of k being observed in the old 

pre-migmatite amphibolites. In contrast to the dike metadiabasic 

amphibolites/ they are characterized by a log-normal distribution of k. The 

great scatter of k values in-' hese rocks indicates that the magnetite 

mineralization is superimposed/ evidently related to granitization.

From the results of petromagnetic investigations of the Archean rocks to 

the northeast of the Pechenga structure it was established that in this region 

there is a systematic relationship between k and the extent of preservation of 

the granulite mineral parageneses. H-igh k are typical of enderbites- and 

charnockites/ which in essence are shadow migmatites of the granulite facies. 

During diaphthoresis of the epidote-amphibolite and amphibolite facies/ the 

magnetite in these rocks disappears or its content is sharply reduced to 

values typical of similar rocks in the section of hole SD-3/ in which the
10 - a , A/m

Fig. 11.16. Magnetic susceptibility of the main Archean rock 

types in the section of hole SD-3 and of the drilling area as 

a function of natural remanent magnetization.

On the surface: 1 - biotite gneisses with garnet, 2 - highalumina gneisses, 3 - biotite gneisses with epidote, 4 - crystalline schists and amphibolites, 5-7 - rocks of granitization 

series I diorites, tonalites, plagiogranites, diaphthorized 

to various degrees, 8 - rocks of granitization series II, plagiomicrocline granites-granodiorites.

In the hole: 9 - figurative field of rocks of the section in 

hole SD-3 in the 7-10 km interval (80% of measurements yield 

Q < 2).

150
maximum extent of appearance of Lower Proterozoic metamorphism-diaphthoresis 

is recorded for the Archean formations.

If the values of k measured on core samples are compared with those 

obtained by borehole magnetometry, it is established that they practically 

coincide, i.e. the suggestions of some investigators that pressure has a 

substantial effect on k is not supported by the results of the investigations 

in hole SD-3. Thus the conditions of occurrence of the rocks (at least in the 

upper part of the earth's crust) do not affect k; therefore, it is correct to 

measure it at atmospheric conditions on core samples and to use those values

as the true values.

According to the data of statistical treatment of a large number of 

measurements of magnetic susceptibility, two regularities in its distribution 

in the section are ascertained (see Table 11.11):

 down-hole from the Proterozoic rocks to the Archean gneisses, k

-3 -4 av decreases systematically from 10 to 10 SI units, except for the

-2 

peridotites of the Zhdanov formation (sedimentary sequence IV, k}10 ) and

the magnetite-rich zone of the Pirttijarvi formation (volcanogenic sequence 

II, k>10~3 );

 with depth, the difference between average values of magnetic 

susceptibility of the igneous and sedimentary rocks evens out. In sequence IV 

(Zhdanov and Materta formations) it still happens, but beginning with sequence 

III (Zapolyarna and Luchlompol 1 formations) and below, the average values of k 

in these rocks already are no different (k =8.10 SI units), except 

for the magnetite zone in volcanogenic sequence II.

Both regularities are in agreement with the increasing extent of 

metamorphism with depth from prehnite-pumpellyite and greenschist facies to 

epidote-amphibolite. The process of deep metamorphism on the one hand is 

usually accompanied by destruction of the magnetic minerals, and on the other 

by chemical equalization of the composition of the rocks.

The results of comparison of the average values of k for the petrophysical 

intervals distinguished indicates the informativeness of k for lithologic 

subdivision of the section. The Student t-criterion was used as the 

statistical criterion of the difference.

The anisotrophy of magnetic susceptibility and remanent saturation

magnetization J of the rocks varies greatly (k / . up to 2.9, 

rs 3 max/mm r

J ^rg in UP to ^* 4 ^ ' reacni n9 a maximum in the schistose parts of the 

section of the magnetite zone of the Pechenga Complex and especially in the
Archean gneisses. The great scatter of values of anisotropy is explained in 

part by the random sampling of the orientation of recovered samples with 

respect to the directions existing in the earth's crust. The following 

regularities were ascertained relative to anisotropy: 1) a general increase 

in anisotropy downward; 2) the anisotropy within a sequence is higher in the 

sedimentary than in the igneous rocks (igneous rocks 1.05, sedimentary 1.21). 

Evidently this is related to the greater schistosity of the sedimentary rocks 

compared to the igneous. This difference levels off with depth, which is 

consistent with the increase in extent of metamorphism.

Thus, the magnetic anisotropy is paragenetically' related to the elastic 

anisotropy of the rocks it increases with depth and extent of regional 

metamorphisra.

NATURAL REMANENT MAGNETIZATION -J

n

As a result of the fact that the core of hole SD-3 was not azimuthally 

oriented, it is impossible to analyze in detail the behavior of the total 

vector J ; only the values of its absolute value value J and the angle 

between the vector J and the horizontal plane, I, was considered

(inclination of the vector J ).

n

The value J has a lognormal distribution even in the most uniform 

n

petroraagnetic groups of rocks and depends primarily on the magnetite content 

and superposed pyrrhotite mineralization of metamorphic origin.

The maximum value of J , 21,610.10 A/m, was recorded in the

n

serpentinized 'peridotites of the Pechenga Complex, which are rich in magnetite 

and pyrrhotite.

In the Archean rocks penetrated by the hole, J as a whole is lower than 

in the Proterozoic formations, but the contribution of remanent magnetization 

to the total is often much greater than in the rocks of the same type in the 

Archean complex northeast of the Pechenga structure at the surface, which 

again is related to the pyrrhotite mineralization typical of most of the 

section of hole SD-3.

Normal polarity of the J vector predominates in the section of hole 

SD-3. The average values of inclination I for rocks with relatively high Q 

(carrying pyrrhotite mineralization) are clustered in the 30-50° range (fig. 

11.17). With a decrease in Q the inclination is shifted toward larger 

angles, i.e. it approaches the inclination of the present geomagnetic field 

(on the order of 80°). Thus the less stable rocks were partially or wholly
10

O o

o 

e 

 * o

CD

o

o o

..

JT,degrees

Fig. 11.17. Relationship between average values (for

the ouitec^- of inclination of the vector

magnetization and the Koenigsberg ratio for' the suites-^ /cr /* »<*

1 - Materta, Zapolyarnaya; 2 - Zhdanov, Luchlompol ' and 

PirttijSrva, 3 - Kuvernerninj ok , Majarva, 4 - Archean 

formations.

153
remagnetized under the influence of the present geomagnetic field. Such 

unstable rocks are most common in the first volcanogenic sequence (Materta 

suite). The stability of the average inclinations of J of rocks with a 

high Q throughout the section and their difference from the inclination of the 

present field and similarity to the inclination of inversely magnetized rocks 

indicates that such rocks retain ancient remanent magnetization.

As the scatter of values of inclination is not large, it can be presumed

that the age of the remanent magnetization J is approximately the same

n

throughout the section.

THE KOENIGSBERG, ' RATIO Q

The Q factor is the ratio of natural remanent magnetization to induced, 

and is very important for interpreting magnetic anomalies. In the section of 

hole SD-3 it varies from 0.1 to 29 and correlates with the composition of the 

magnetic minerals: in the zone of pyrrhotite mineralization, high Q are 

observed, and in the magnetite zone Q is less than 1.5. It should be 

mentioned that in the sedimentary rocks of the pyrrhotite zone, Q as a 

rule is higher than in igneous rocks, due to the prevalence in the former of 

magnetically harder material antiferromagnetic pyrrhotite. The relatively

high Q for such ancient rocks indicate that the J is thermoremanent or 

av n

chemoremanent.

Normal polarity of the J vector predominates in the section. The total 

thickness of inversely magnetized rocks is about 10%.

According to the data of borehole magnetometry, the zones of pyrrhotite

»

and magnetite mineralization are different. The zones of sulfide 

mineralization (pyrrhotite) are marked by serrated, sharply angular magnetic 

anomalies (up to 5.10 nTll, the anomalies of the horizontal component 

considerably exceeding those of the vertical (about 1.5 times greater). No 

According to the data of borehole magnetometry, the Q factor is up to 40 

units.

The zone of oxide (magnetite) mineralization is marked by more intensive 

and less angular magnetic field anomalies (up to 10-20 Ips nTl), which 

correlate very clearly (fig. 11.18) with intensive magnetic susceptibility 

anomalies (up to 500.10 SI units). The relative contribution of remanent 

magnetization to the total in this zone is much less than for the zone of 

sulfide mineralization, the q values in this zone are on the order of 0.1-1.

154
\v

Za -10, nTl

Fig. 11.18. Correlation of the vertical component 

of the magnetic field 2a and magnetic susceptibility < for zones of magnetite mineralization, according to data of borehole magnetometry.

TABLE 11.12

RESULTS OF INTERPRETATION OF MAGNETIC 

LOGGING DATA

Interval ,

m

4600 4616

4880 5640

5717 5720

7628-7633

9640 9655

Dip of

1 P "%/f> T* C

Azissuth

of rH r>

degrees

35

65

35

70

50

200

150

150 '130

170

155
 -. %. A

M--

The angles and azimuths of the dip of the magnetic layers are given in 

table 11.12 on the basis of data " * interpretat£T fVtsw the magnetic logging 

readings.

The data of table 11.12 indicate angular and azimuthal unconformities in 

the attitude of the zones of magnetite mineralization. The sharp 

discontinuities manifested in the density, elastic and other properties of the 

rocks are also observed in the magnetic characteristics.

Results of magnetic-miner alogical analysis of the rocks. The saturation

magnetization, determined by the composition and content of ferromagnetic

2 minerals in the rocks, varies widely from 0.05 to 15.9 A.m /kg, even in

the case of the same rock types and a small sample volume. This suggests an 

extremely uneven distribution of ferromagnetic minerals, which can only mean 

superposed mineralization. Low values of J 0.2 A.m./kg prevail in

5 w

volume, especially in the lower part of the section. This fact, together with 

the data of thermomagnetic analysis with the hyperbolic shape of the 

J (T) curve is a sign of low concentration of ferromagnetic minerals and 

large contribution of paramagnetic iron minerals to the magnetic effect.

According to thermomagnetic analysis and study of the coercivity spectra 

it is established that two kinds of pyrrhotite are present in the rocks 

studied: ferromagnetic (monoclinic) and antif erromagnetic (hexagonal) type.

In the thick magnetite zone of sequence II, where pyrrhotite is 

practically absent, the magnetite concentration varies from 0.5 to 17%, 

judging from the value of J The Curie points vary from 580 to more than

S

600°C. This is related to the monophase oxidation of magnetite and formation 

of cation-deficient magnetite, which is confirmed by data of X-ray phase 

analysis. Beneath the magnetite zone, in the Archean rocks at a depth of 

7.2-10.5 km, magnetite is present everywhere along with pyrrhotite (according 

to thermomagnetic analysis, T_ = 580-620°C) .

Against a background of general increase in temperature downward from

sequence IV to II, from greenstone to amphibolite metamorphism, zones of

Alow- temperature magnetization are observed in the lower part of sequences III,

I and the Archean. The observed inhomogeneity probably suggests repeated 

pyrrhotite mineralization (or recrystallization) , in particular 

low-temperature.

On the basis of these criteria, it is easy to distinguish superposed 

processes involving the lower part of the gaobro body (depth 1282-1421 m) and 

the peridotite bodies (550-570 m and 1540-16/0 m) and the country rocks
adjacent to them. The oldest generation I of pyrrhotite mineralization is 

distinguished at depths of 500 m or more (gabbro to 1282 m). The later 

generation II was superimposed on the lower part of the gabbro (depth more 

than 1321 m) and underlying country rocks. Variations in the magnetic 

properties of pyrrhotite as the peridotite body is approached indicate that 

this body (1540-1670 m) is younger than generation II and correspondingly 

younger than the gabbro. The pyrrhotite mineralization involving the lower 

part of that peridotite body and the country rocks adjacent to it is the next 

generation, III. The pyrrhotite occurring in the peridotite body at a depth 

of 550 m and in the rocks enclosing it should be assigned to it. Pyrrhotite 

generation IV is distinguished in the country rocks above the contact with the 

gabbro body situated at a depth of 1987 m. Toward the contact of this body 

the magnetic properties of the pyrrhotite do not vary. The exceptionally 

narrow and intensive/\-peaks of those pyrrhotites suggest that this is the 

best preserved and possibly youngest mineralization.

From the results of study of the magnetic characteristics of the'rocks in 

the borehole, determined on core samples and from logging data, the following 

conclusions can be drawn:

1) large scatter of k and J values is found in a small volume of rock,

n

which indicates the superposed character of the mineralization;

2) the difference between mean values of k and J of the sedimentary and

n

igneous rocks evens out with depth; beginning with sequence III, Proterozoic, 

the average k values for these rocks are the same;

3) the peridotites of sequence IV and the volcanics of Proterozoic 

sequence II, where high magnetite concentrations are observed, stand out 

sharply.

4) the section is divided into three zones on the basis of magnetic chaj 

racteristics: depth interval 0-4586 corresponds to the zone of sulfide

mineralization. The rocks of this zone are mainly weakly magnetic, the 

average values of magnetic susceptibility do not exceed 4.10 SI units, 

except for intervals of ultramafic rocks. The existence of an intensive 

magnetic field in the zone is related to remanent magnetization of pyrrhotite 

and magnetite. The main magnetic mineral of this zone is pyrrhotite, except 

in the ultramafics, in which magnetite is present in large amount; 

 depth interval 4586-5642 m corresponds to the zone of oxide 

mineralization and is characterized by higher magnetic susceptibility of the

rocks, up to 0.2-0.3 SI units; magnetite, cation-deficient magnetite, and 

hematite are present;
 depth interval 5642-10,500 m is a zone of development of weakly 

magnetic rocks. The magnetic susceptibility values reach (2-4).10 only in 

isolated places; small concentrations of pyrrhotite and magnetite are 

observed;

5) The average inclination of the J vector with relatively high Q,

n

considerably different from the inclination of the present geomagnetic field, 

and also the variations in magnetic polarity of the rocks (regardless of their 

composition and magnetic mineralization) indicates the ancient origin of the 

natural remanent magnetization. About 20 zones of different geomagnetic

polarity are recorded in the section. The average inclination of the J

n

vector of the rocks studied is similar throughout the section and does not 

correlate with the magnetic anisotropy; thus the age of magnetization of the 

rocks containing pyrrhotite and magnetite is similar;

6) on the basis of several magnetic properties/ several types of magnetic 

mineralization are distinguished, differing in conditions and time of 

formation: a) disseminated pyrrhotite mineralization in the sedimentary rocks 

of sequences III and IV; b) disseminated pyrrhotite mineralization in the 

mafic igneous rocks of sequences III and IV; c) "ore" pyrrhotite 

mineralization, later than the first two, confined mainly to the endocontact 

of a peridotite body and fractures in the sedimentary rocks of sequences IV 

and III; d) disseminated pyrrhotite mineralization in sequences I and II and 

the Archean gneisses/ evidently relatively the latest (low-temperature); e) 

mineralization produced by enrichment in magnetite during serpentinization of 

the peridoties of sequence IV, close in time to the "ore" pyrrhotite 

mineralization; f) hematite-magnetite mineralization of sequence II/ the 

relative position of which in time is not clear; evidently it occurred before 

pyrrhotite mineralization of sequences I and II and/ the Archean rocks; judging 

from the temperature of magnetization of magnetite (above 500°C), it was 

produced earlier or at the same time as the amphibolite facies metamorphism;

7) crystallization, transformation and magnetization of the pyrrhotite and 

magnetite are closely related to the metamorphism of the rocks.

RADIOACTIVITY OF THE ROCKS

NATURAL RADIOACTIVITY

The natural radioactivity of the rocks of the section in the hole was 

studied both on core and in the hole. On core, the content of natural 

radioactive elements (NRE) uranium/ thorium and potassium was
determined. For this purpose the following methods were used: laboratory 

gamma spectrometry; scintillation gamma-spectrometry; instrumental neutron 

activation analysis for uranium and thorium; X-ray spectral and X-ray 

fluorescence analyses; delayed neutron. The average contents of NRE were 

determined for the rock types ascertained in the petrochemical investigations.

In the hole, the radioactivity of the rocks was determined by gamma 

logging both in the integral (GL) and spectrometric (SQL) versions.

Proterozoic

The rocks of this part of the section fall into four groups on the basis 

of natural radioactivity.

In the first group there are rocks characterized by very low total natural 

radioactivity (less than the average clarke contents). On the basis of the GL

interval readings, the rocks in this group have a natural radioactivity

14 (intensity of Y radiation I__) averaging (7.9-15.8).10 A/kg. The second

GL

group includes rocks in which the total radioactivity (from GL) averages

14 (14.3-32.3).10- A/kg; the third group includes rocks with a natural

14 radioactivity of (40.8-79.5).10 A/kg. The fourth group is characterized

14 by maximally high readings for the middle Proterozoic (79.6-133.4).10

A/kg (from GL).

The rocks of groups I and IV can be unambiguously distinguished by gamma

14 logging. Radioactivity values of (14.3-79.6).10 A/kg (groups II, III)

are typical of rocks of different composition and origin, in connection with 

which the parameter in question is not informative for subdividing the rocks 

of those groups.

The possibilities of using natural radioactivity as a parameter for 

recognizing the rocks of the Middle Proterozoic are, greatly increase^ if gamma 

logging data are examined together with the contents of the individual NRE in 

the rocks in specific parts of the section. For this purpose, it is most 

feasible to determine the natural radioactivity by formations.

In the Materta formation, mainly magnetic rocks of basic composition are 

developed. The spread of GL readings (including SGL) for them is small. 

However, the character of the curve is different for individual rocks. For 

the gabbro diabases uniform GL readings throughout their thickness is

typical. In the basalts and diabases, which also are considerably thick, the

14 readings in individual parts of tne section increase to (14.3-21.5).10

A/kg, which apparently may be elated to the inclusion of small intercalations
V*

of tuffogenic sedimentary rocks in the diabases.

In the GL readings, tuffs of basic composition, picrite and pyroxene 

porphyrites are hardly different from the diabases and gabbros. but the 

contacts between these rocks are rather clearly established from GL data.

A high information content of natural radioactivity in subdividing the 

section is typical of the Zhdanov formation.

In this formation, a group of mafic and ultramafic rocks (group "a") is 

unambiguously distinguished, in comparison with which the rest of the rocks of 

the formation differ essentially in radioactivity values.

To ascertain the ultramafics, other methods should be used, including 

determinations on core and mud. Gamma spectrometrie data (SGL) in combination 

with the readings of other methods provide additional material for 

distinguishing zones of considerable alteration

(serpentine-talc-chlorite-tremolite rocks) in the ultramafics, in which the 

content of uranium and thorium is higher.

Separation of the sedimentary rocks (group "d") is extremely difficult 

because of the macro- and microinterbedding of sedimentary formations of

A

different grain size. However, varieties with a prevalence of phyllites are 

distinguished from essentially siltstone varieties by higher contents of 

thorium and potassium.

In the Zapolyarna formation, volcanogenic-sedimentary rocks (group "b") 

which occur among diabases and tuffs of basic composition (group "a") are 

distingished on the basis of gamma logging data. The latter can be 

distinguished on the basis of SGL readings: higher contents of thorium and 

uranium are typical of the tuffs.

The rocks of the Luchlompol' formation are similar in content of 

radioactive elements and are the most highly radioactive of the Proterozoic 

formations. The integral readings of gamma activity of these rocks also are 

very similar to each other, but on the basis of SGL data these rocks can be 

clearly divided on the basis of the higher contents of uranium and thorium and 

relatively low potassium in the andesite-dacite porphyrites compared to the 

arkosic sandstones.

Subdivision of the rocks of the Pirttijarvi formation can be done on the 

basis of the total radioactivity values, based on gamma logging data.

The sedimentary-metamorphic formations of the Kuvernerin formation are 

divided into originally chemogenic-sedimentary and chemogenic with an

admixture of clastic-sedimentary material on the basis of gamma logging.

=- 160
t The rocks of the Maarva formation/ the most metamorphosed of all the

A 

Proterozoic formations, are distinguished from unmetamorphosed rocks of the

same composition on the basis of radioactivity values.

NUCLEAR-PHYSICAL PARAMETERS

The nuclear-physical characteristics of the rocks in the section of SD-3 

were determined in situ by the methods of GGL-S [selective gamma-gamma 

logging], PNNL [pulsed neutron-neutron logging] with thermal and epithermal 

neutrons.

For conducting borehole investigations of crystalline rocks at 

considerable depths in the section of SD-3, examples of PNNL and GGL-S 

apparatus were developed, built and modernized on the basis of standard IGN-4 

and DRST-2 instruments.

For the first time ever, measurements were made by a dual-probe PNNL 

apparatus (probe length 40 and 90 cm) at depths to 8000 m at high temperature 

(T - 140°C) and high pressure (p r 100 MPa) simultaneously at three time lags 

(800, 1000, 1300 microsec) and in an interval regime on each probe. Data were 

obtained on the average life time of thermal neutrons.

The nuclear-physical parameters of the crystalline rocks were determined 

from the results of chemical analysis of cores.

On the basis of integrated investigations, conclusions were drawn 

concerning the relationship of IT values and effective atomic number of the 

rock Z to their mineralogical composition, and a procedure was developed 

for interpreting the PNNL and GGL-S data.

Fig. 11.19 shows Z - as a function of the total content of iron and 

calcium (Fe+Ca) in the Archean crystalline rocks in SD-3 (at depths greater 

than 6842 m), and fig. 11.20 shows the dependence of, the parameter of the 

macrosection of thermal neutron capture Z'c to the total content of iron and 

boron in the rocks Fe+B ('in equivalent % of Fe content) . According to the

data of calculations of z ,- and 'C the Proterozoic and Archean rocks in ef

SD-3 fall into three groups (table 11.13), taking into account silicic content 

and the inverse relationship between the silicon and iron contents (fig. 

11.21).

The first group includes diabases, gabbro-diabases, essexite gabbros; 

actinolitized and arnphibolized diabases and gabbro diabases'; porphyroblastic, 

plagioclase-amphibole, and magnetite-biotite-plagioclase-amph:ljv_le schists and 

rocks; pyroxene porphyrites, pyroxene metaporphyrites, serpentinized
2 ef

ffh

;j

72

2,0

1,5

1,0

Fe*B,%

Fig. 11.19. Effective atomic number Z ef as a function of total content of iron and calcium in the 

rocks (%Fe).

Fig. 11.20. Dependence of the parameter of macrocross-section of thermal neutron capture z c ' on total content of iron and boron in the rocks 

Fe+B (%Fe).

Fig. 11.21. Relationship between 

mass contents of iron and silicon in 

in crystalline rocks.

Fe, %

TABLE > 11.13

NUCLEAR-NEUTRON PARAMETERS AS A FUNCTION 

OF ROCK COMPOSITION

Rock

roup

1

2

3

Rocks

Mafic, ultramaf ic

Intermediate

Acid

*.f

15 17

13.5 15

12 14

T, usec

110 260

260 380

380 500

162
peroditites, serpentine-chlocite-talc rocks; amphibolites ,

plagioclase-amphibole, and magnetite-biotite-amphibole-plagioclase rocks and

schists.

The second group consists of rocks of intermediate silicic content, 

quartz-plagioclase schists with amphibolite, biotite-arapbibole-plagioclase 

schists and gneisses, leucocratic and melanocratic, with high-alumina 

material, actinolite-talc rocks, and oligoclasites.

The third group includes andesite-dacite porphyrites, potassic and sodic 

granites and granite gneisses.

The statistical distribution of the z - and ~ parameters by rock group 

are also given in fig. 11.22. The experimental values of the parameters z f 

and tf are defined in the form of continuous histograms down the section of 

SD-3 using selective gamma-gamma (GGL-S) and pulsed neutron-neutron logging 

(PNNL).

Thus study of the natural radioactivity and nuclear-physical properties of 

the rocks on core from SD-3 and logging data made it possible to: establish 

the content of natural radioactive elements (NRE) for certain types of rock in 

the hole and enhance the detail of subdivision of the section; distinguish 

zones of high NRE content related to secondary alteration of the rocks, in 

particular to granitization;- ascertain the regularity of an increase in 

natural radioactivity with increasing depth; and use data on nuclear-physical 

properties to determine the petrographic composition of the rocks in the 

section.

THERMAL PROPERTIES OF THE ROCKS

Study of the thermal properties on core samples in the drilling area was 

necessary to obtain reliable data on the thermal field in the area, and also 

to predict deep temperatures on the basis of the thermal conductivity 

equation, where the parameters of thermal conductivity determine the rate of 

the process of heat transfer to the surface.

Several methods were used to measure the thermal properties of the rocks

2 

 heat conductivity [W/(m.K)], temperature conductivity k (m /s) and

heat capacity C [J/(kg.K)]: 1) flat instantaneous source to measure K,C, k; 

2) comparative on plates 40 mm in diameter and 6-10 mm thick; this method was 

used to measure ^small samples or when , ^values were high; 3) dividing 

rod [bar?J-~ in measurements on small samples (plates 21.5 mm in diameter, 

3-6 mm thick); 4) noncontact determination of heat conductivity using a moving

163
a 

n n 

40

20

11 13 75 , Zef 100 300 OTTt, MS

Fig. 11.22. Statistical distribution of the parameter Z ef (a) and t (b) 

in rock groups 1-3 (corresponding to table 11.24).

164
point source; 5) thermal comparator with two-point probing of surface of 

sample.

The last four methods are used only to measure the heat conductivity 

coefficient. On the basis of control measurement (more than 40) made on the 

same core samples, it was established that the comparability of results of 

measurement of A in the 1.5-4.5 W/(m.K) interval for methods 1-4 lies within 

3-15%.

For rocks of the Pechenga Complex the thermal properties were measured by 

methods 1-4 on core samples of all the main rock types, collected to a depth 

of 6842 m. Core samples in an air-dry state were used. To a depth of 1700 m 

the samples were taken not only from the super-deep, but also from other 

holes. The heat conductivity values are given in fig. 11.23.

From table 11.14 it is seen that the maximum values of heat conductivity 

for igneous rocks [A= 4.27-5.23 W/(m.K)j were obtained for the andesite 

porphyrites (group VI) and schists of various compositions (group VII), which 

can be explained by the high content of minerals with high heat conductivity 

in the samples: up to 50% chlorite [A = 5.2 W/(ra.K)] or carbonate [A = 3.6- 

5.8 W/(ra.K) in schists and up to 60% quartz [A= 7.7 W/(m.K)] in andesite 

porphyrites with low (up to 10-20%) content of albite [ x\ = 1.9-2.3 W/(m.K)]. 

The minimal values are characteristic of amphibolites collected from a depth 

of more than 5 km [group III,/\ = 1.38 W/(m.K)*] and serpentinized

ultramafic rocks of the Zhdanov formation [group IV, ,\ = 1.84 W/(m.K)].

av

For core samples of group II (H = 2805-4500 m) the extremes of variation

and average values of heat conductivity [^ = 3.8 W/(m.K)] are somewhat

av

higher than for samples of slightly altered rocks taken from lesser depths [^ 

= 2.7 W/(m.K)]. The differences in values obtained in measurements along the 

axis and perpendicular to it do not exceed 4%. Belpw 4500 m lies the boundary 

between the greenschist and"amphibolite facies of metamorphism, and the 

massive rocks of the upper part of the section are succeeded by schistose. 

The heat conductivity of the metabasic rocks below this boundary is sharply 

different from the heat conductivity of the rocks of basic composition in the 

upper part of the section. For the rocks of group III (more than 5000 m deep) 

^ is sharply lower [^ = 2.3 W/(m.K), and the values obtained in 

measurements along the core axis and perpendicular to it differ by 12% on the 

average. Such substantial reduction in heat conductivity [compared to /\ =

«V

3 W/(m IT, ] evidently is related not only to the mineralogic conversion of 

ir.o 1 ite [ A = 3.8 W/(m.K)] to hornblende [ ^ = 2.5 W/(m.K)], but also to
H,*.M

J

2

J

4

S

1 S

7

Lithoibogic

r nl mnn

L L L

L^L^L

k. k.

L^L^L

/^ / > <^

L U

i^*,^fc^r*/^ jr*^^r»n

ISHS--^

V V

^% /^ /^ /-\

f*\ f\ f\

r r r

 5?^ ?PSr~

:: ;:a:-:.'^';: :<?:-:

r r r

IL^JZ^-vC.

L^L^t

L I

L t t

LAtAt

^r^r^

L L t 

L L

L^L^t ^ k- k -

-s^^ ^ ^

V V V

V V V 

V V

V V V

 _i -!

< < <

< <: < 

< <

.'.o. : . «. . -aA,W/(tn-K)

2 J 4

 .

 

 * *

 *

 * "

 * 

* 

9

*

9 

 * *

 * *

 *'*.

 4 «

« * * 1 

 * *»«. «

*J * .

* 

^ «

 

* * 

* * * *

 * 

f > . 

Fig. 11.23. Heat conductivity in the Froterozoic section 

For symbols in lithologic column, see appendix <

c.h

166
TABLE 

LIMITS OF VARIATION AND AVERAGE VALUES OF THE THERMAL PROPERTIES (K, C, X) AND DENS

SAMPLES OF THE MAIN ROCK GROUPS OF THE PECHENGA COMPLEX

cr.

Rock

Gabbroids - . .

Metagabbro-diabases

Amphibolites .

Serpentinized ultra-.

mafic rocks

Tuffs - ... 

Andes! te porphyries

Schists

Sedimentary and . .

tuf fogenic-sedimentary

rocks

/r, £/<:** *

Limits of 

variation

2b6-3I2

2.80-3!27

2.92-3.13

2.85-3.13

2.84-3.10

2.80-3.07 

2.69 3.05

2.96 3.01

2.72 2.91

2.72-3.17

60

M 

0)

3.00

3.04

J.03

2.92

2.93

2.92 

2.78

2.99

2.84

2,8f

A' n»". n'/i

Limits of 

variation

0.88 1.43

0.83-1.43

0.98-1.24

0.84-1.18

1.01 1.41 

1,52

1.62

1.03 1.77

.0

QJ 

60 

tti

0)

1.09

1.07

1.09

1.03

1.15

1.32

c- /<«/'

Limits 

of variation

630-880

630 1170

670-1090

670-920

670-920 

840

920

750 1000

K>

Averagej

800

840

840

800

840

920

a

a

0^

cl 

&w

10

41

24

5

5 

5

4

10

44

x.

6

2 22

2.22

2.42

1.38

2.05

1.84

2.55 

3.26

3.0

2.66

2.13

I'ftM

1

3.01

3.18

3 68

3.14

3 89 tJ ( Ui*

3. CO

2.93 

4.27

5.23

3.91

3 93

K)

average)

2.70

2.70

3.00

2 29

2.97

2.55

2.74 

3.50

3.86

3.22

3,00
textural and structural changes occurring during metamorphism, which 

corresponds to a change in elastic properties.

For the sedimentary rocks, the highest values of /\ were obtained for 

quartz-mica, arkosic sandstones [/\ = 3.8 W/(m.K)] and quartz-mica siltstones 

[>= 3.2-3.5 W/(m.K)] .

Thus the average values of heat conductivity of the rocks of the

Proterozoic complex are 2.3-3.9 W/(m.K)] (see table 11.14). For the 

volcanogenic rocks of this complex, the correction for moisturejis negligible.

Considerable anisotropy of heat conductivity was ascertained (in dry and 

water-saturated rocks). The maximum values of were recorded for profiles 

oriented perpendicular to the schistosity or linearity, and minimum with 

values parallel orientation. Heat conductivity anisotropy in gneisses and 

schists in general is in good agreement with the elastic anisotropy in the 

same rocks.

On the whole, the results of integrated study of the thermal properties of 

all rock types in the continuous section of SD-3, which penetrates the major 

structural-formational zones of the Baltic shield (Pechenga paleo-caldera of 

Proterozoic age and underlying Archean Kola complex), indicated a zonal 

distribution, -- ^

GEOTHERMAL INVESTIGATIONS 

HEAT FLOW AND ITS CHARACTERISTICS

The most important characteristics of the thermal field of the earth's 

crust are the geothermal gradient ^ (GTG), heat conductivity /\ , heat flow 

density (HD) in the near surface zone, and the distribution of sources of 

radiogenic heat A. The geothermal gradient is determined by measuring 

temperature after an equilibrium state of the thermal regime is established in 

the hole. In the case of horizontal beds and steady-state heat conductivity 

regime, heat flow is determined as the product of the GTG and thermal 

conductivity of the rocks, q = y/S. Thus the dependability and reliability of 

heat flow calculation depend on the precision of determination of ^ and /). At 

present, y is measured with a precision of about 5%, and A of 7-10% (for an 

actual well section). The complexity of obtaining sufficiently precise values 

of ^\ is related to the fact that the measurements are not made in situ, but on 

core samples. In determining/\, the effect of water content of the rocks 

especially at depth, must be taken into account. At depths of 5-10 km a 

substantial part of the pores and fractures are closed. The real values of 

heat conductivity in low-porosity crystalline rocks at depth as a rule are 

higher than the values obtained under laboratory conditions.
Before drilling SD-3 in the Pechenga structure, 10 holes 470-1675 m deep 

were studied. The GTG in holes that had been standing for a year or more, 

heat conductivity of core samples/\ , and heat flow density q were determined.

The values of q were determined by interval-by-interval averaging of the

data on the gradients and heat conductivity 7\ . To a depth of 1000 m ^ d av _. av

the average value q is (26+2) W.m , in the 1000-2800 m interval it is -2 3V 

(36+4) W.m . At a depth of 5000 m the average value of q drops and falls

-2

within 48-56 W.m . It should be noted that the decrease in q occurs only

from a depth of 6800 m. Very low values of the flow in the upper part of the 

section (to a depth of about 1 km) can be explained by the effect of several 

factors: filtration, glaciation not long ago, and denudation. 

RADIOGENIC HEAT IN THE THERMAL BALANCE OF THE EARTH'S CRUST AND UPPER MANTLE

The heat flow generated due to decay of radioactive elements (RE) in the 

earth's crust, and the heat flow arriving from the upper mantle, are 

determined on the basis of an accepted model of the structure and composition 

of the crust, and also the character of distribution of uranium, thorium and 

potassium in it. The distribution of the average contents of the RE by rock 

type and sequence in the section, and also radiogenic heat in the Proterozoic 

and Archean rocks, are of special interest.

Pecbenga Complex. fa "fc/a/ tff 532 analyses for uranium, thorium and

!

potassium contents were made for the rocks of the Pechenga Complex. The lower 

formations were sampled in less detail than the upper, in connection with the 

low core recovery beginning at a depth of 4600 m. However , all the main rock 

varieties were sampled, and in determining the average contents of RE by 

formation, the readings of the GL and GL-S geophysical methods were taken into 

account.

The Materta and Zapolyarna formations, which consist mainly of diabases

and metabasic rocks, had the minimum contents of uranium, thorium and

 > 

potassium, and the Zhdanov and Luchlompol' formations, the maximum. The high

RE contents in the Luchlompol 1 formation are explained by the presence of a 

body of andesite porphyrite, characterized by a relatively high content of U, 

Th and K. Low RE contents in the Kuvernerinjok formation are caused by the 

rather extensive occurrence in it of low-radioactivity carbonate-tremolite 

schists.

When the average values of the RE in the volcanic flows are compared, a 

tendency is noted toward a decrease in their content downward from the Materta

formation to the Zapolyarnm: (to a depth of 4673 m). Below that an increase in

169
RE contents is recorded. The high contents of RE in the Pirttijarva formation 

are related to its complex composition: in addition to metabasites, 

intermediate and silicic effusives are extensively developed here 

(metaandesites and metaalbitophyres), characterized by high RE contents. In 

the Maj'arva formation, which consists mainly of basic effusives, the high RE 

contents are explained by superposition of processes of foliation,-

metaraorphism and granitization.

Kola Complex. The Kola complex, Archean, was subdivided into sequences by 

co-workers of the KGRE and VSEGEI on the basis of lithologic criteria, taking 

into account superposed processes of polymetamorphism. The following features 

were taken into account in the subdivision: presence of rocks with 

high-alumina minerals; relative content of biotite-plagioclase gneisses and 

amphibolites; extent of granitization.

It was presumed that despite the intensive manifestation of superposed 

metamorphism, the primary details of the rocks are still partially preserved 

at least in their mineralogical composition. For instance, the presence in 

the rocks of high-alumina minerals (silliraanite, staurolite, andalusite) 

unambiguously indicates the original pelitic nature of the metasediments. Six 

sequences are distinguished on the basis of the features cited.

The average RE contents in the sequences depend to a considerable extent 

on the degree of granitization of the rocks and the quantitative relationship 

of granites and pegmatites, silicic and basic varieties.

HEAT GENERATION

From the vertical distribution of values of heat generation to a depth of 

11,400 m (fig. 11.24) it is seen that its character depends mainly on the 

particulars of lithologic composition of the Pechenga and Kola complexes. A

maximum level of heat generation characterizes the tuffogenic-sedimentary t - .

rocks (1.0-2.5 ^W/ms) and essexite-bearing gabbro-diabases (0.7-1.7 ^iW/ms), 

which are developed mainly in the upper part of the section of the series, to 

a depth of about 2.5 km. Below that, in the region of preferential 

development of intensively metamorphosed mafic volcanics (in greenschist and 

epidote-amphibolite facies) the heat generation value falls on the average to 

0.04-0.08/X. w/m . An abrupt increase in heat generation in narrow intervals 

at a depth of 3700-4700 m is related to thin intercalations of tuffites and 

andesite porphyrites, respectively. The peak of heat generation at a depth of

4700 m may be caused (in addition to the lithologic factor) by the thick

170
1,28

Matsrta'

"hdanov

1053 -

2

2805 H

Zapolyarna . ^

Jfff73 -

Luchloinpol' 

Pirttl.la.rva SSM

 Cuvernerin 1 ok

Malarva

-j -nclr 6823

0)

o

c

0)

a 

cr a) w

S8U2 

7522

6 -

MS 5

3579 H 

W

10600 -

nuw -

J2 -

Fig. 11.24. Variations in heat generation in the section of SD-3-.

1^- heat generation by suites*and sequences; 2 - variations in heat generation within suites: depth distribution of heat generation: 3 - Ukrainian

shield, 4 - Sierra Nevada batholiths. 

*

171
highly permeable zone of the Luchlompol ' fault, like the abrupt increase in 

heat generation at a depth of about 9500 m, where a highly permeable weak zone 

is recorded in which (on the basis of analysis of the contents of primary 

helium) it seems possible that elements have been brought in, including 

radioactive ones .

It is important to note that in the mafic volcanogenic rocks of the 

Pechenga complex, which are similar in chemical composition but metamorphosed 

to different extent, the RE contents vary widely (by more than an order of 

magnitude) , which probably is caused by the particulars of the behavior of 

uranium in the course of progressive metamorphism. The value of heat 

generation of the volcanogenic sequences of the Pechenga complex is about 0.4, 

of the sedimentary about 1.3^W/m '.

In the Archean Kola Complex the value of heat generation in the two-mica 

gneisses (amphibole-plagioclase) with high-alumina minerals is close to the

, 0

value of that parameter in the sedimentary sequences (1.2-1.7 uW/irn}; in the 

sequences of the more basic varieties of gneisses (amphibole-plagioclase) with 

intercalations of amphibolite it is appreciably lower and amounts to about 0.8 

. Thus as a result of the investigations, no systematic decrease in

heat generation values with depth was found. The vertical distribution of 

heat generation is step-wise in character, determined mainly by the 

mineralogical composition of the rocks. '

For comparison, average curves of the deep distribution of heat generation 

are given for the Precambrian Ukrainian shield and the Sierra Nevada 

batholiths, which are Mesozoic. The absolute values of heat generation for 

those regions fall in similar intervals (about 0.2-2/{W.m ) calculated for 

the Kola hole. It should be noted that the vertical distribution of heat 

generation in lithologic varieties of the same type, (individually for 

metabasites and tuf fogenic-sedimentary rocks of the Pechanga complex) is close 

to an exponential distribution law.

MODELS OF HEAT GENERATION

In correspondence with present ideas on the structure of the crust in the 

Pechenga region, it is advisable to consider two models of heat generation.

Model I. According to this model the lower boundary of the 

"granite-gneiss" layer of the crust runs at a depth of 12.5 km where, 

according to the data of vertical seismic profiling, there is a discontinuity 

in the crust which has not yet been unambiguously interpreted. On the one

172
hand, it may be a region of transition from amphibolite to granulite facies 

metamorphism, and on the other, it may reflect the lower boundary of 

distribution of the zone of granitization in the crust.

In this model, the Proterozoic sedimentary-volcanogenic Pechenga 

(developed to a depth of 6842 m) and Kola complexes can be attentively 

assigned to the "granite-gneiss" layer. The latter consists (according to the 

data of the drilling of the Kola hole to a depth of 11612 m) of rocks of 

varied composition (both silicic and basic) In the drilled part of the 

section, six sequences of different composition have been distinguished. A 

uniform lithologic composition of the section is presumed to the distinguished 

discontinity (12.5 km). Below that boundary, to a depth of 40 km, there 

apparently is the "granulite-basite" layer, concerning the composition of 

which there are different opinions.

This model is based on the idea that this layer consists of metabasic 

rocks of different metaraorphic facies (amphibolites, pyroxene granulites, 

eclo~gites) . Depending on the proportions of "dry" granulite and 

water-bearing amphibolite facies in the composition of the layer, heat 

generation may vary from 0.2 to 0.6 ^W.m . An average value (0.4 MW.m :) 

was used in the model. The calculation of that model shows that the 

radiogenic heat sources in 'the crust generate a heat flow of 23 ^W.m (the 

rest of the flow comes from the mantle).

Model II. According to this model it is presumed that the section of the 

Kola Complex of gneisses, analogous to the section penetrated by the hole, 

continues to a'depth of 15 km, below which (to a depth of 20 km) rocks 

corresponding in composition to the varieties constituting the Murmansk block 

are present (the so-called basement of the Kola Complex) . This part of the 

section of the crust (to 20 km), tentatively including the Pechenga complex, 

is identified with the "granite-gneiss" layer. Below that, to a depth of 40 

km, there is the "granulite-basite" layer. In this model (in contrast to 

model I) , two sublayers are distinguished (in depth intervals of 20-30 and 30- 

40 km) within the "granulite-basite" layer, on the basis of DSS data. The 

contents of radioactive elements and heat generation in these sublayers are 

taken on the basis of the clarke values in the rocks of corresponding 

composition (respectively, gabbro-amphibolite for the upper sublayer and 

granuli te-eclogi te for the lower). The radiogenic component of heat flow in

the cru^w calculated for this model differs slightly from the results obtained

-2 

with se'*«l I, being 26 ynW.m- , which is 45-55% of the total surface heat

2 flow measured in SD-3 (49 >4iW/m ).
Thus the following are established on the basis of the results of the 

geothermal investigations.

1. The geothermal gradient increases with depth from 1-1.1°C/100 m in the 

upper part of the Pechenga complex to 1.7-2°C/100 m in the lower part (at a 

depth of 6000-7000 m). The variation in the GTG with depth evidently is 

related to variations in heat conductivity, heat generation and water content 

of the horizons.

2. In the Proterozoic section heat flow increases with depth in 

connection with an increase in the content of radioactive elements.

3. The vertical distribution of heat generation (according to the 

constructed model) varies step-wise with depth, which is caused by the 

lithology of the rocks.

4. The radiogenic component of heat flow in the crust is 45-55% of the 

total surface heat flow measured in SD-3.

PHYSICO-MECHANICAL PROPERTIES

The physico-mechanical properties of the rocks in the section of SD-3 were 

determined only on core and were used mainly to solve technological problems 

of drilling. The following characteristics were determined: static Young's 

modulus E,t ; static Poisson'.s ratio v ; compressive strength 0^ ; 

tensile strength O* ; resistance to indentation (hardness) ?j_n ; plasticity

K ,; and abrasivity z. pl

The determination of p. , K , and E. (from indentation of die) was

rin pl in

accomplished on. YMGP-3 and UMGP-4 instruments according to GOST-12288-66. In

addition, E. and v. were measured on these same instruments in a regime in in

of quasi-uniaxial loading of a cubic sample, with measurement of the 

deformation over its whole length. Abrasivity z was determined by the 

procedure of wearing down the flat rock surface with1 a steel rod.

The strength characteristics of rocks most widely used are the critical 

strength under conditions of very simple loading schemes- uniaxial 

compression and tension. These characteristics are obtained by splitting off

a number of slices 15x30x100 and subsequently crushing samples (cubes about

A 

15 mm on edge). For each sample at least 15 slices were made, from the

results of which the tensile strength was calculated, and at least ten cubes 

were crushed to determine the compressive strength. The results of the 

individual determinations in each sample were treated statistically in 

accordance with the hypothesis of critical distribution [26].

174
It should be noted that according to the generally accepted procedures, 

determination of the strength of rocks specifies cutting slices at least 30 mm 

thick and crushing cubes 40 mm on edge. Inasmuch as it was not possible to 

use samples that size due to the poor core recovery in SD-3, the feasibility 

of extending the methods of slicing and crushing the cubes to small samples ' 

was checked. As a result of experiments on optically active materials, the 

predominant action of tensile stresses in splitting slices 10-15 mm thick with

wedges was confirmed. Comparison of the results of determination of <5* for £f>

homogeneous pyroxenites showed that the values obtained on very small samples 

are comparable to those obtained on larger ones (fig. 11.25).

The strength characteristics of the core of SD-3 are extremely variable 

inasmuch as they depend on a large number of decisive factors, including the 

mineralogical composition, structural-technical particulars of the rocks, 

fracturing (healed) and microfracturing.

The main factor governing the variations in strength characteristics of 

the upper part of the Pechenga Complex to a depth of 4500 m is the 

petrographic-mineralogic composition of the rocks. The critical compressive 

strength for the rocks of this part of- the section varies from 114 MPa in the 

talcized picrites and peridbtites to 219 MPa in the diabases (table 11.15), 

the latter value being the maximum for the whole section in hole SD-3. The 

critical tensile strength varies from 22 MPa in thin-bedded metasedimentary 

rocks to 45 MPa in diabase. In the bedded sedimentary rocks, anisotropy of 

the strength properties is clearly manifested. For instance, in phyllites the 

tensile strength a" is 32 MPa measured perpendicular to the bedding and 40 

MPa along the bedding.

In the lower part of the Pechenga Complex (to a depth of 6800 m) the 

average values of compressive>strength <^-/ 160 MPa, are not very different C-p

from the corresponding parameters in the upper part. The meta-leucodiabasic 

amphibole-plagioclase schists have V = 15 MPa under tension transverse to 

the schistosity and 24 MPa along it. Thus the strength of these rocks, which 

are the commonest in the 4900-6800 m depth interval, is 2-3 times less than in 

the diabases and metadiabases which constitute a large part of the upper 

Pechenga subcomplex. Anomalously low strength parameters characterize the 

chlorite and talc-chlorite metadiabasic and metapicritic schists, lying in the 

4500-4673 m interval.

175
cu ,MPa

130

TOO

CO 200 

"of saraple

Fig. 11.25. Cotnpressive strength of 

rocks as a function of length of sample,

2000 MPa

Fig. 11.26. Correlation between strength of rocks and hardness to indentation: a - tension, b - compression. Dashed lines designate confidence 

intervals.

Fig. 11.27. Correlation between elasticity 

modulus upon indentation Ei±a and modulus of 

of deformation under uniaxial compression

£2 in

TABLE 11.17

ABRASIVITX 'OF ROCKS PENETRATED BY SD-3

Rock

Phyllites

Chlorite-sericite and talc^ized rocks

Porphyrites, peridotites, diabases, gabbrodiabases, sandstones, gneisses

Tuff, granites, crystalline schists

Class

I

II

IV

V

Abrasivity 

characteristics

Below average

rr rt

Average

Above average

176
TABLE 11.15

AVERAGE VALUES OF THE PHYSICO-MECHANICAL PROPERTIES OF THE MAIN ROCK TYPES 

OF THE SECTION IN SD-3

Rock 8,

g/cnr

<*p <'s

kmps

V

^dyn10 "'- 

MPa

a* MPa

J L«. | JtE

tp ;>

MPa

Apl

Pechenga Complex 

Ma terra suite (0-1059.. m).

Diabases 

Tuffs

Komatiites

Phyllites,

siltstones

Interbedded sandstones, 

siltstones, phyllites

Tuffs, tuffites

Amphibolitized and chloritized gabbro-diabases 

Essexite gabbrodiabases

Serpentinized 

peridotites

Metadiabases, green

schists

^leta-picritic talc-chlorite 

schists with hematite 

Tremolitized dolomites

Tuffs, tuffites v

3,02 

(1987) 

2,92 

(582) 

3,03 

^359)

6,80 

(63) 

6,48 

(34) 

6.28 

(23)

3,66 

(60) 

3.50 

(31) 

3,23 

(23)

1,02 

(63) 

1,05 

(34) 

1.04 

(23)

10,4 

(61) 

9,1 

(31) 

8,8 

(23)

0,27 

(61) 

0,28 

(3!) 

0,29 

(23)

45 

(7) 

41 

(5) 

26 

(4)

45 

(7) 

41 

(5) 

26 

(4)

219 

(7) 

153 

(5) 

114 

(4)

27,8 

(24) 

29,6 

(6) 

17,3

(6)

2,3 

(24) 

2,7 

(6) 

2,0 

(6)

Zhdanov suite* (1059-2805 m)

2,90

(1457)

2,84

(1297)

2,88

(325)

2,98

(1948)

2,84

(552)

2.88

(627)

6,03

(54)

5,91

(48)

6,20

(18)

6,24

(52)

5,92

(15)

6,29

(17)

3.41

(50)

3,59

(42)

3.48

(17)

3.56

(50)

3.32

(13)

3,49

(15)

1,06

(54)

1,10

(48)

1,08

(18)

1,03

(52)

1,02

(15)

1.02

(17)

8,0

(49)

8,8

(44)

8,7

(17)

9,3

(50)

8,1

(13)

9,0

(15)

0,20

(49)

0,20

(44)

0,27

(17)

0,24

(50)

0.27

(13)

0,27

(15)

32

(7)

22

(10)

32

(4)

29

(8)

28

(4)

30

(5)

40

(7)

26

(10)

36

(4)

30

(8)

28

(4)

35

(5)

183

(7)

122

(10)

116

(4)

179

(8)

175

(4)

190

(5)

15,7

(16)

14,9

(3!)

11,9

(4)

27,7

(20)

35

(3)

17,7

(8)

2.3

(16)

2,0

(31)

2.4

(4)

2,0

(20)

2.0

(3)

2,3

(8)

Zapolyarna suite''(2805-4673 m)

3,02

(5630)

2,93

(192)

2,88

(130)

6,58

(214)

5,46

(8)

6,18

(4)

3,76

(216)

3,35

(6)

3,66

(3)

1,04

(214)

1,35

(8)

1.14

(4)

10,6

(216)

8,2

(6)

9,6

(4)

0.23

(216)

0,22

(6)

0,24

(3)

30

(35)

6

(1)

10

(3)

31

(35)

10

(1)

46

(1)

175

(35)

29

(1)

126

(1)

35,3

(112)

3.8

(11)

24.4

(4)

1.6

(112)

2,1

(ID

1,7

(4)

Luchlompol 1 suite* C4673-4884

Dolomite and sandy 

dolomite

Arkosic sandstones 

Andesite-dacite

metaporphyri r «.<?

Serpent inized 

peridotites

2,77 

(55)

2,78 

(214)

2,75

(259)

2

, 9.9. *o

(627)

5,25 

(2)

5,22

(10 

5.47

(9)

6,29 

(17)

3,41 

(1)

3.20 

(10) 

3.39

(9)

3,49 

(35)

1,08 

(2)

1.12 

(11) 

1,11

(9)

1.02 

(17)

6,6 

(I)

6.6 

(9) 

7,5

(8)

9.0 

(15)

0.05 

(1)

0,15 

(9) 

0.16

(8)

0.27 

(15)

 

22 

(0

30 

(5)

22 

(1)

36 

(5)

161 

(I)

190 

(5)

13,4 

(1)

21,8 

(10) 

21

(7)

17.7 

(8)

1.4 

(I)

1.8 

(10) 

1.9

(7)

2.3

(8)

177
Table 11.15, continued

Rock a

g/cm3

' s

, K.IUUO kmps

*,' %m lft

MPa

*

<*£,, MPa

 t «t1

Qc* p .

/>

MPa

A pl

Pirttijarva suite (4884-5619 m)

Magnet ite-bio tit e-amphibole schists after trachybasalts

Magne tite-b io tite-plagioclase schists after trachyandesite basalt

2.97

(315)

2.86 

(244)

5.80

(18)

5.04 

(20)

3.50

(13)

2,96 

(5)

1.13

(18)

1.14 

(20)

7,8

(ID

6,1

(4)

0.18

(11)

0.20 

(4)

__ __ _ _. 28

(21)

20.5 

(2)

2.3

(21)

2,3 

(2)

Kuvernerlnjok suite (5619-5717. m)

Tremolitized dolomites 

Meta-diab?_sic amshib elites

Carbonate-mica

metapsammites

2.85 I 

(55)

2.74 

(87)

6.10 

(3)

5.32 

(6)

3,12 

(2)

3.22 

(5)

1.11 

(3)

1,10 

(6)

7.1 

(6)

6.5 

(6)

i

0,22 

(C)

 *" " 12.2! 

(3)

21,6 

(5)

3.1 

(3)

2.0 

(5)

Majarva suite (5717-6835 m)

Amphibole-plagioclase 

schists after leuco-diab«aoe

Quartz-bio tite-plagioclase

schists after andesites

Meta-diabasic amptiibolites

2,90 

(1895)

2.78

(15)

3,03

(122)

5.28 

(79)

5,28

(1)

5.76

(4)

2,91 

(86)

2 go 

, oo

(1)

3.26

(6)

1,14 

(79)

1.12

(1)

1.08

(4)

6,1 I 

(44)

5,7

(1)

7.6

(4J

0.21 

(44)

0.23

(1)

0,23

(4)

15 

(5)

_

_ _

' 

34 

(5)

__

.

160 

(5)

_

_

20.4] 

(78)

29.4

(1)

16.4

(7)

2,2 

(78)

1,6

(1)

1.8

(7)

Archean Group

Sequence I, gneisses with high-alumina minerals (6842-7622 m)

Biotite-gnej.sses with highalumina minerals

Migmatite-granites , 'pegmatites

2,77 

(241)

2,64

(223)

4,29 

(12)

4,34

(5)

2,54 

(1)

_... .

.18 

(12)

1,97

(5)

3,4 

(12)

3,5

(3)

0.01 

(1)

_

 ~

11.5

(1)

117

(1)

12 

(10)

22,3

(7)

3,3) 

(10

2.7

(7)

^Sequence II, shadow migmatites, gneisses and amphibolites (7622-9456 m)

Shadow migmatites, 

gneis s-plagiogranites

Plagiomicrocline

gneiss-granifp.s

Epidote-biotite, epidotebiotite-amphibole gneisses

and schists

Amphibolites

2,65 

(5245)

2.62

(241)

2 78

(328)

3.02

(417)

3.99 

(40)

3,50

(4)

4.34

(4)

4.62

(10)

1,84 

(15)

1.83

(4)

1,89

(10)

1.05 

(40)

1.05

(4')

1 08

(4)

1.13

(10)

2,02 

(15)

1.6

(4)

2,3

(10)

0,17 

(15)

0,20

(4)

_

0.13

(10)

7 

(8)

__

9.5

(1)

5

(1)

11 

(8)

__

21

(1)

20

(1)

194 

(9)

_

151

(1)

27,8 

(42)

375

(4)

23,1

(4)

25,8

(7)

0 0

(42)

2.0

(4)

2,8

(4)

2.0

(7)

Sequence III, two-mica gneisses with fibrolite (9456-9541 m)

Two-mica

 gneisses with

fibrolite

2.72

(98)

178
Table 11.15, continued

Rock g/cm]

*P *s

kmps

*.'

MPa

»

a t ,MPa

 ti tit

 cp "in

MPa

«PI

Sequence IV, shadow migmatites, gneisses and amphibolites (9541-10,144 m)i

Shad ox* migmatites ,

gneiss-plagiograniteson^aShadow mi2mati t"«?«

Epidote-biotite , epidolebiotite-amphibole gneisses

and schists, migmatized

plagiomicrocline granites

Amphibolites

Blastocataclased, chloritized shadow migmatites

Blast oca ta'clased, chloritized amphibolites

2.68

(1118)

2.67

(318)

3.00

(411)

2,65

(219)

2,96

(183)

4.03

(3)

4,24

(3)

4.98

(2)

5,96

(3)

2,55

(1)

"

1,06

(3)

1.24

(3)

1.05

(2)

1.12

(3)

1.3

(3)

~

0.05

(3)

 .

 . ~

 «_

 

_ .

 

~

^_

_

~

__

__

 "*

22,8

(5)

17.6

(6)

28,2

(5)

25

(6)

0 0

(5]

2.4

(6)

1.8

(5)

2.0

(6)

.Sequence V, two-mica gneisses with fibrolite (10,144 to 10,600 m)

Two-mica gneisses with 

fibrolite

Amphibole-biotite gneisses 

granodiorites 

Gneiss-granites n^d 

pegmatites, plagiomicrocline

2,70

(1683)

2,66

(427)

2,62

(93)

3,02]

(2)

3,30

_

__

__

1,22

(2)

1,06

(1)

_ .

_ .

_

__ ^

_

1_ IM1I

_

...

-

_ .

i

__

_

__

ilMII

13.41

(13)

14,3

(2)

20,9

(3)

2,1 

(13)

2.0 

(2)

(3)

Sequence VI 

Shadow migmatites

Epidote-biotite-ainphibole gneisses, schists

, shadow migmatites, gneisses and amphibolites (10,600-11,000 m)

a f-ff-o c 2.64 ___ _ _ _ _ i9 ( s 1,8

(»*) _-.-.-. - - - - - (2) (2)

2.97 3.63

(43) (3) (3)

18,9 1.9 

(1) (1)

Low-er Proterozoi c -Archean(?)

(Dike?) complex of orthoamphibolites and ultramafic orthoschists (6,842-11,000 m) 

Meta-diabasic amt>hibolites

Meta-leucodiabasic amphibolites, including cummingtonites

Phiogopite-talc-tremolite schists after 

ultramafic rocks

Remarks: In parentheses - number of measurements

3.06

(1209)

2.92

(1120)

2,94

(77)

4.75

(13)

4,42

(15)

4.27

(4)

2.25

(4)

2,6o

(3)

1,91

(1)

1.18

(13)

1.12

(15)

1.21

(4)

3.48

(6)

3.40

(3)

2,6

(1)

0,20

(4)

0.04

(3)

0,19

(I)

13

(2)

11

(3)

5

(2)

18

(2)

23

(3)

11

(2)

182

(2)

190

(3)

64

(2)

26.5

(22)

22 8

(12)

7,5

(5)

2.2

(22)

2.2

(12)

2,1

(5)

179
In the Archean complex the critical compressive strength varies from 64 

MPa in the phlogopite-talc-tremolite schists, which are sporadically 

developed, to 182-194 MPa in the commonest rocks of the section shadow 

migmatites (gneiss-granites) and amphibolites. In the Archean rocks the tr 

values vary from 5 MPa in the phlogopite-talc-tremolite schists, transverse to 

the schistosity, to 23 MPa in the amphibolites along the schistosity, i.e. 

they are appreciably lower than the O* of the rocks of the Lower 

Proterozoic.

Prom Pig. 11.26 there is seen a clear correlation of elastic properties of 

the drill core with critical tensile strength. There also is a relationship 

between elastic anisotropy and strength anisotrophy of the rocks recovered 

from the hole. This interrelationship is based on the phenomenon of partial 

disintegration of the core upon decompression. Therefore, the strength 

indices, at least of the lower part of the section, cannot be used to 

calculate the true strength of the rocks penetrated by SD-3 in situ.

During drilling, information was constantly needed as the rocks were, 

penetrated, especially their strength, which necessitated using a rapid 

procedure for calculating the strength of the rocks along with determining the 

critical compressive and tensile strength. The fastest method is 

determination of the mechanical properties of the rocks under conditions of a 

volumetrically stressed state using the indentation method.

The mean weighted values of hardness under the die for the rocks of the 

Pechenga Complex is 2520 .MPa (Table 11.16), with variations from'380 MPa in 

the meta-picritic talc-chlorite schists (4578-4673 m) to 3530 MPa in the

metadiabases. The values of P. (indentation hardness) in the metamorphosed in

tuffogenic-sedimentary rocks (1190-2180 MPa) are appreciably lower than in the 

metamorphosed magmatic formations (1640-3530 MPa), except for the 

blastomylonites of greenschist facies, rich in chlorite, mica, talc and 

serpentine, developed after mafic and ultramafic rocks, which are 

characterized by anomalously low values of indentation hardness.

The mean weighted value of P. for the Archean complex is 2230 MPa, i.e. 

just a little less than .that given above for the Proterozoic. The 

phlogopite-talc-tremolite schists (750 MPa), and biotite and two-mica gneisses 

with high-alumina minerals (1200 MPa), common in the 6842-7622 interval, have 

low p.. The shadow migmatites and amphibolites, most common in the Archean 

part of the section, have p. = 2780 and 2570 MPa, respectively.
TABLE 11.16

AVERAGE WEIGHTED (BY THICKNESS) VALUES OF PHYS I CO-MECHANICAL PROPERTIES OF 

THE ROCKS OF THE SECTION IN HOLE SD-3 BY SUITE, SEQUENCE AND COMPLEX

suiter

sequence , 

complex

Suite:

Materta

Zhdanov

Zapolyarna

Luchlompol1

Prittijarvi

Kuverneriniok

Majarvi

Pechenga

sedimentar'

volcanogen: 

complex as

a whole

Sequence:

I-gneisses 

w . hign-AI

minerals* .

II -shadow migmatites

gneisses & 

amphibolite

III-two-mic

f

neisses w,

ibrolites

IV- shadow

migmatites

gneisses &

amphibolite

V- two-mica

f

neisses w

ibrolites

VI-shadow

migmatites

gneisses &

amphibolite

Archean

amphibolite

migmatitegneiss complex (including

orthoamphibolites)

as a whole

H, M

0 1059

1059 2805

2805 4673

4673 4884

4884 5619

5619-5717

5717-6835

0 6842

c

6842 7622

7622 9456

s

a 9436 9541

9541 10144

;

10144 10600

10600 11000

>

6842 11000

<n«6 

oo

00

3,00

2,90

3,01

2,76

2,92

2,80

2,91

2,94

2,75

2,73

2,72

2,77

2,72

2,65

2,73

»P vs

kmps

6,68

6,09

6,50

5,36

5,47

5,79

5,33

6,08

4,29

4,12

3,56

3,50

3,73

3,35

3,26

3,16

2,94

3,45

2,54

1,85

4,26:1.65

3,20

3,32

3,99

_ _

2,17

if * 

1,03

1,05

1,05

1,11

1,13

1,11

1.1-1

1.07

1,16

1,07

1,09

1,20

1,06

1.10

£dyd0 * 3' 

MPa

10,0

8,7

10,4

7,1

7,0

6,9

6.3

8,7

3,4

2,4

2,8

 _ _

2,7

>

0,27

0,23

0,23

0,14

0,19

0,22

0,21

0,23

0,01

0,16

0.08

__

0,11

at, MPa

<VK7

42

28

28

22

__

77

_

42

32

31

22

_

ISO*

'

 ' 

 

J_mu_

*cp In

MPa

195

162

164

161

_

192C

__

26,8

20,4

33

20,1

24.8

16,5

20.4

25,2

140

2&J

220

153

195

223

V

2,-J

2,1

,7

,8

2,3

2.o

2 2

2JO

2,<J

2,2

2,1

2,1

1,8

2.2

*A11 calculations orthoamphibolites taken into account. 

**Limit of tensile strength £ determined in two directions: perpendicular cr tj_ and parallel a^i to bedding and schistosity.

181
On the basis of correlational analysis (see fig. 11.26) it was established 

that the values of indentation hardness are closely related to the values of 

(jr . and less closely to <?*.. The correlation coefficient r in the first 

case is 0.89, in the second 0.35 (confidence interval at the 1% level of 

significance r - 0.56). In addition, from the results of the analysis it was 

established that the effect of the decompression factor on the index p. of 

the core is secondary, the main role belonging to the mineralogic composition 

of the rocks. However, it would not be right to completely deny the role of 

decompression, as the indentation hardness of rocks of the same type at the

surface is 20-30% higher than the p. values measured on core recovered from in

depths of 7-11 km.

It is known that the ratio of critical compressive and tensile strength

characterizes their brittleness (plasticity): the higher theC£_/0~ ratio,

'rr A

the greater the brittleness and correspondingly the lower the plasticity of 

the rock. The most brittle rocks have a ratio of ^./^ = 15-20.

The brittleness of the rocks penetrated by the hole to a depth of 6842 m, 

i.e. to the Archean basement, is low on the whole. Some increase in 

brittleness is recorded in the lower part of the Pechenga Complex, for 

instance for the amphibcle-plagioclase schists. The brittleness of the rocks 

recovered from depths greater than 6842 m is still higher. For this part of 

the section decompression has more effect on the physical properties of the 

rocks than the mineralogic composition.

The coefficient of plasticity determined by the indentation test .is 

theoretically the value inverse to the brittleness of the rocks. However, no 

rigid correlation between the coefficients of plasti ity and brittleness of 

the rocks was recorded, as the indices obtained in the indentation test depend 

to a much greater extent on the mineralogic composition of the core than on 

the extent of its partial .disintegration.

To ascertain the more complete characteristics of the physico-mechanical 

properties of the rocks of the section in SD-3, data of determinations of

E and E , obtained in a regime of auasi-static uniaxial stress of the dyn st

sample with a measure of deformation along its whole length were compared. 

The results of the comparison (fig. 11.27 [p. 41]) showed that the value of

the modulus E .is less than the value of E, for all rocks of the same _st dyn

mineralogical type, but the character of variation of E, and E through dyn s <_

the section is practically the same: maximum values of E ^ , as of E , ^ * st dyn

are observed in the upper part of the section (diabases and gabbro-diabases of 

volcanogenic flows IV and III), where E_ = (5.0-7.5) .10+ Mpa.
The E, /E , ratio for the different rock types proved to be Q jf n s c

different: for diabases and gabbro-diabases it is 2, and for sedimentary 

rocks 1.7, which is in agreement with the variation in plasticity of the 

rocks.

To solve technological problems, the abrasitivity Z of the rocks plays a 

large part.

The average values of abrasitivity of the rocks in the section in SD-3 

vary from 3 to 48 mg. It is known that the abrasivity of crystalline rocks 

with respect to steel is larger, the greater the microhardness of the minerals 

entering into the composition of these rocks. However, in the case of 

friction additional roughness arises in polymineralic rocks, related to the 

difference in resistance to abrasion of the minerals, which leads to an 

increase in abrasivity which is particularly noticeable for clastic rocks. 

The minimum abrasivity, as would be expected, is that of phyllites, 

chlorite-sericite and highly talcized rocks (Z = 3-16 mg), the maximum, of 

granites, amphibolites and crystalline schists (Z = 46-48 mg). Owing to the 

effect of additional roughness, tuffs, tuffites and sandstones are 

characterized by high abrasivity (Z ='24-44 mg).

According to the classification of rocks by abrasive properties, the rocks 

investigated fall into four classes (table 11.17).

Thus as a result of study of the physico-mechanical properties of the 

rocks of the section in SD-3 it is established that:

 the section consists mainly of elastic-plastic rocks of high 

strength and average abrasivity;

 the character of variation of the strength properties through the 

section is very uneven, due to which serious complications arise during 

drilling, and routine evaluation of these properties is constantly needed, 

using a rapid procedure for corrective drilling regimes:

 the procedure of determining hardness of the rocks by indentation with 

a flat base best satisfies the requirement for rapidity; the results of

hardness determination correlate well with the indices of compressive and

»

tensile strength.

 the physico-mechanical properties of the rocks depend (by analogy with 

the acoustic properties) on these factors: petrographic-mineralogic; 

decompressional (it is of decisive importance in the lower part of the 

section).

183
The most informative parameter in estimating the stability of the walls of 

the hole is tensile strength, which decreases down-hole in jumps, and relative 

to which anisotropy of the rocks is manifested.

VERTICAL ZONING OF PHYSICAL PROPERTIES OF THE ROCKS AND

CRQSTAL STRUCTURE FROM THE RESULTS OF STUDY OF THE SECTION AND THE

AREA OF THE KOLA SUPER-DEEP BOREHOLE

The results of drilling, geophysical investigaions, study of core samples 

recovered at the surface, and also data of geological and geophysical 

investigations in the immediately adjacent territory provide the possibility 

of approaching problems of the general structure of the earth's crust in a new 

way.

One of the most pressing but least studied and debatable problems in earth 

science is the question of systematic variations in physical properties at 

great depths. An unambiguous answer to this problem is possible only by using 

the results of super-deep drilling and petrophysical models (Footnote 1: 

according to the definition of Ye. V. Karus and L.V. Shierina, a petrophysical 

model means the distribution at depth of physical characteristics determined 

in a single hole.) of the section. Study of the petrophysical models is 

necessary to enhance the precision and uniqueness of ground geophysical 

surveys.

ELASTICITY-DENSITY MODEL

The main regularity ascertained in studying elastic and density 

characteristics in the section of SD-3 is the fact that the maximum values of 

density O* and longitudinal and transverse wave velocities, v and v , and <y

lr O

also minimal porosity are observed in the upper part of the section. A sharp

decrease in v , v_ and ff and an increase in anisotropy of the rocks is P S

observed at a depth of 4500 m in a sequence of rocks of the Zapolyarna 

formation, uniform in composition (fig. 11.28). The first discontinuity 

(depth 4500 m) almost coincides with the boundary between the greenschist and 

epidote-amphibolite facies metamorphism, the second with the boundary between 

the Archean and Proterozoic. Below the first boundary schistose rocks occur 

everywhere.

Attention should be paid to the fact that at the boundary of the upper and 

lower groups of the Lower Proterozoic, the coefficient of anisotropy of

elastic wave velocities^increases in a jump, increasing within one member from

184
Suite"

Materta

Zhdanov

Zapolyarna

Lucnlompoj

KuverA 

nerinjq

Maj Srvi

Tele-\ 

Vinsk«,

Archean 

group

Lithologic

column

U- U -I.

r: r:

/.J

eo c '

1 l\

1.28.. Elastic and density properties of the rocks of the section in SD-3 

For symbols in lithologic colunm, see append^.

185
1.06 to J.37. Below 4500 m the coefficients of anisotropy vary widely/ 

reaching 1.6, but not one member returns to the values of the upper group of 

the Middle Proterozoic, i.e. does not exceed 1.05-1.09.

For the section in SD-3, ideas of an increase in velocity with depth for 

rocks of the same composition were not supported. Such factors as, for 

instance, progressive and dislocational metamorphisin leading to structural 

alterations in the rocks affect the elastic properties: maximum velocity 

values are observed in the upper part of the section, i.e. there is an 

inverted seisraogeologiq section (velocity inversion).

In the Archean formations there is observed a distinct division in density 

and velocity of the amphibolites and gneisses, and the upper high-alumina 

sequence of gneisses is denser than the lower. Below this boundary, no 

increase in anisotropy of the rocks relative to elastic properties is 

observed.

SEISMOACOUSTIC MODEL 

Using modern acoustic logging apparatus in SD-3, a detailed velocity

section for longitudinal v and transverse v_ waves was obtained, vertical

p S

time-distance curves of these waves were plotted, effective damping was

i 

determined and taking into account the density of the rocks, a seismoacoustic

model of the section was compiled (fig. 11.29). The main feature of this

model is that to a depth of 4500 m, no gradient in v and V G velocities is P S

present; below that there is observed a local negative gradient, indicating 

some decrease in velocity (according to data of acoustic logging and vertical 

seismic profiling). When the vertical time-distance curves plotted on the 

basis of the results of these different-in-principle methods of CIS [?] are

compared, complete similarity of the data practically throughout the section *o*-

is obtained, except the very lowest part where the quality of the acoustic

A

logging material is much worse than for the upper part of the section. 

It should be mentioned that the sharply expressed zone of inversion

(decrease in v and v velocities) is observed from the readings of the P s

CIS method just as clearly as from the data of core measurements. However, 

due to the effect of the attitude of the rocks on the velocity of propagation 

of elastic waves, the P values determined from acoustic logs are higher than 

the results of core measurements, even if the latter are water-saturated (see 

fig. 11.29). For dry samples this difference is still more considerable. 

From the acoustic logging a«'ca, as from the core, the velocity changes 

abruptly at a depth of 4500 m (from 6.8-7 to 5.5-5.8 kmps). 186
Vertical timedistance curves

Fig. 11.29. Seismoacoustic model of the sectionin SD-3.

Acoustic logging data: 1 - reliable, 2 - unreliable: vertical seismic profiling data: 3 - VNIIYaGG, 4 - LGI.
Effective 

coefficient 

of damping 

of waves 

8 01 s,k aj

Fig. 11.29, continued

188
68T

group Archean 

1,1

T<< < 

Suite

Member

Lithologic 

column

OQ

I I 

ro

C

a 

a-

< 0- 

a> Hif en 

O D 

P» O 

rt O 

h^ C 

3 n 

A, I

ID «***!>»- 

cn n o o 

^h O t-h < 

^-h ft) 

n> t-h D. g 

n i-h t» PJ 

n- H- S < 

H- n -o n> 

< H- H- 03 

(D rt S 

3 OP 

rt
Thus, as a result of the investigations made, the presence of a zone of 

inversion of the elastic (and density) properties of the rocks is demonstrated.

The seismoacoustic model of the section was the basis for experimental 

determinations and analytical calculations of the complex stress state in the 

upper part of the crust penetrated by SD-3. The main purpose of these 

investigations was to calculate the attitude of the rocks, which was needed to 

solve geological-technical drilling problems. The conclusion obtained 

concerning the uneven distribution of stress with depth and the presence in 

the section of a thick (about 3 km) zone of considerable easing of stress (to

40 MPa) (Fig. 11.30) is important also for solving geological-geophysical 

problems, in particular ascertaining the possible nature of deep seismic 

discontinuities. Fig. 11.30 gives the results of study of the temperature 

gradient and heat flow in SD-3, the stress state and secondary transformations 

of the rocks. When the results obtained are compared, it is established that 

the boundaries of abrupt change in the stress state of the rocks (curves II 

and IV) correspond to stepwise variation in temperature gradient (curve I) and 

heat flow (curve III) and coincide with the intersections of the section with 

metamorphic fronts and seismic boundaries, and both have a tendency to smooth 

out with depth.

Most investigators believe that the causes of redistribution of stresses 

in the crust are manifold. The results of tectonophysical modeling confirm 

that idea (see Fig. 11.30). However, in the literature it is shown that 

horizontal tectonic forces are manifested only in the upper part of the crust 

and do not affect the vertical component of stresses & . Fig. 11.30 gives 

the variation through the section of precisely that a* component, 

calculated theoretically (curve IV) taking into account the effect of weak 

layers, and determined by the full-scale method (curve II). The results 

obtained by these methods indicate that Cf is nonlinearly distributed 

through the section; there are places both with understressed and overstressed 

rocks (see Fig. 11.30). The principles of redistribution of stresses in all 

probability is governed by internal processes occdrring (or having occurred) 

in the crust, and primarily by metamorphism of the rocks.

The variation in petrophysical characteristics of the rocks with 

increasing intensity of metamorphism changes the character of their 

deformation, and the sharpest changes are recorded in the region of transition 

from greenschist to epidote-amphibolite facies, where massive textures of
Thermodynamic conditions of occurrence of the rocks

Geologic-seismic 

profile

 - _ Mr r r 5 v vff .-..

Fig. 11,30. Correlation of thermodynamic conditions of occurrence of the 

rocks with the locations of boundaries of facies (subfacies) of metamorphism 

and seismic boundaries in the section of Precambrian rocks of the Baltic 

shield penetrated by hole SD-3.

Indices of curves and corresponding scales of measurements: I - temperature 

gradient, °C/100 m, II - vertical component of tensor of stresses (full-scale 

measurement, MPa, III - heat flow, W/m2 , IV - vertical component of stress 

(analytical calculation), MPa. 1 - diabases, 2 - picrite porphyrites, 3 - 

tuffs, 4 - tuffites, 5 - gabbro-diabases, 6 - peridotites; 7 - breccias; 8 - 

siltstones, phyllites, sandstones; 9 - diabases, pillow lavas, actinolitized; 

10 - plagioporphyrites; 11 - dolomites, sandstones; 12 - meta-andesites; 13 - 

orthophyres, albitophyres; 14 - metadiabases; 15 - amphibole schists after 

basalt and amphibolites; 16 - high-alumina gneisses; 17 - plagiogranites; 

18 - biotite-plagioclase gneisses; 19 - amphobolites; 20 - talc-tremolite 

schists; 21 - biotite-amphibole gneisses; 22 - boundary of facies and subfacies of metamorphism; 23 - seismic reflecting boundaries.

191
metabasites are succeeded by schistose textures. In the lower part of the 

section there is observed intense granitization of biotite-muscovite schist. 

It is these boundaries which are recorded by geophysical (mainly seismic) 

methods (see Fig. 11.29).

Inasmuch as the variation in properties of the rocks occurring during 

metamorphism are related to their recrystallization and change in volume, and 

also to heat flow, those phenomena should be accompanied by redistribution of 

stresses in the massif. To explain the recorded changes in stress it is 

necessary to use the regularities found in the variation of physical (mainly 

elastic and density) properties of the rocks of the section, in particular of 

its three-layer division.

The calculations show that using the real modulus of elasticity and values 

of density of the rocks constituting the section, the presence in the section 

of a zone of unloading equal to 40 MPa can be explained by a relative change 

in volume of the unstressed middle layer, which should amount to 0.08% all 

together. That insignificant change in volume can be completely maintained 

for long geologic time and, as a result, the uneven distribution of the stress 

state in the section will be retained. The relative increase in volume of the 

middle layer (dilatation) may also be related to fracturing of the rocks and 

unevenness of their thermal expansion (due to the change in heat flow). The 

observed phenomenon in all probability arises under the effect of the 

enumerated factors related to secondary transformations and accompanying 

changes in the physical (especially elastic) properties of the rocks. The 

boundaries of a sharp decrease (or increase) in stress would be recorded by 

geophysical methods, including seismic (see Fig. 11.30).

Thus in this case the nature of deep seismic boundaries is caused by 

secondary transformations leading to a change in physical properties and in 

the state of matter of the crust, rather than by lithostratigraphic 

variability of the rocks.

TECTONOPHYSICAL MODEL'

It was shown above that the'stress state of the rocks (its distribution by 

depth) plays a large part in the variations of their physical properties and 

in the formation of geophysical boundaries in the crust. In order to obtain 

additional information on stresses in the region of the Kola superdeep hole, 

tectonophysical investigations were carried out. The object of
tectonophysical analysis was reconstruction of the young and recent tectonic 

stress fields in the region of SD-3 and prediction of them at depth. To solve 

the problem, the decomposition method was used, which permits distinguishing 

the components of the stress field on the basis of a systems approach. They 

are referred to tectonodynamic systems of different scale.

By tectonodynamic system we mean a systematic genetic model of the 

relationship of tectonic movements, deformation and stresses occurring in a 

volume of the lithosphere, the physico-mechanical properties of which can be 

considered to be uniform at the scale of consideration used. Tectonodynamic

systems form a hierachy closely related to the hierachy of tectonic 

deformation (structures). A relationship is established between the size of 

the area of averaging (size of the base on which the measurements are made) 

and the depth distribution of stress fields of a given tectonodynamic system.

To reconstruct stress fields, the systematic relationship between 

orientation of the axes of the principal normal stresses and geometry of the 

spread in orientation of tectonic fracturing, established theoretically and 

confirmed by field investigations, seismogeologic data and modeling was used.

The greatest difficulties in reconstructing young and recent stress fields 

in the region described were related to determination of the age of 

fracturing. Study of aerophotographs, space photographs, and the topography 

of a region taking in the whole northwestern part of the Kola Peninsula, made 

it possible to distinguish faults, clearly manifested in the relief, and thus 

assumed to be rejuvenated or produced in the young stage of tectonic 

evolution. Statistical analysis of the relationship between the length of 

these faults and the average distance between them showed the discreteness of 

distribution of this parameter, i.e. the possibility of distinguishing the 

hierarchy of faults in the region, which presumably belonged to tectonodynamic 

systems of different scale. Plotting of rose diagrams of strikes of these 

faults, which chiefly have steep dips, showed that the faults of different 

scale differ both in general strike and in scatter of strikes. This made it 

possible to suggest that in the area of SD-3 the Regional stress field is of 

strike-slip character with north-northeast orientation of the compressional 

axis and northwest relative tension (Fig. 11.31).

To precisely determine the age of this stress field, the focal mechanisms 

of earthquakes in the whole Arctic region were analyzed (see Fig. 11.32, 11.33 

a, b), which not only made it possible to predict major faults in the area,
V *"

Fig. 11.31. Scheme of the stress 

state of the Arctic rift region 

(a) and rose of strikes of major 

failts of the Kola peninsula from 

data of space photographs, geoloSic surveys and aerial photos.

, , "resa field in

th,e "°"hwestern part of the Kola Peninsula.

Trajectories of axes: 1 - tension, _

2 - intermediate, 3 - compression; Trajectories or axes: 1 -tension, 2 -

4 - presumed faults; 5 - direction compression; 3 - major faults; 4 - minor

r . j * ..i faults. of compression and tension of the

regional field.

Fig. 11.33. Roses of strikes (1) of young tectonic fractures in zones of 

ancient faulting (2).

Joints: a and c = superposed neotectonic, b = "inherited" of young sta/fle.

a

194
coinciding with faults established independently on the basis of geologic, 

geophysical and remote sensing date, but also to confirm the earlier-noted 

orientation of the axes of principal normal stresses. Thus the present stress 

field (seismological data) to a substantial extent has inherited the young (at 

least Holocene) plan of orientation of axes of principal normal stresses in 

the area of SD-3.

The preliminary results thus obtained made it possible to formulate the 

task of detailed analysis of the stress field on the basis of a large number 

of measurements (more than 5000) of tectonic fractures in the Pechenga 

structure and its immediate surroundings. In the deposits of the Pechenga 

complex there were distinguished several systems of fractures having different 

mineral filling. These fractures correspond to old tectonic stress fields. 

In addition to these, fine hair-like or open cracks devoid of mineral filling 

occur everywhere in the region investigated. They form systems, in places 

rather clearly expressed in the present relief, often accompanied by 

slickensides, and they displace all older fractures having a mineral filling. 

The systems of these fractures are parallel lineaments readily deciphered on 

large-scale space photos.

All these signs indicate a young age of the fracturing in question. A 

large number of measurements of fractures were made on a more or less uniform 

grid so as to evenly elucidate all deposits of different age and lithology in 

the Pechenga complex. For each observation point (containing an average of 

100 measurements) a local, stress field was reconstructed. The points were 

joined for surface outcrops of individual formations, groups of formations, 

and finally, for the whole area. Analysis of the sum of data obtained made it 

possible to bring out the stress fields related to the action of 

tectonodynamic systems of different rank, i.e. characterizing different depth 

levels of the crust.

It was established that the lithology of the individual sequences, small 

faults, dikes, boundaries of zones of differently metamorphosed rocks, etc., 

considerably affect the character of the local tectonic stress fields. The 

role of the enumerated factors varies abruptly depending on the structural 

position and orientation with respect to the external stress field of lower 

rank. Thus, young fracturing either completely follows the older structural 

plan, rejuvenating old faults, or cuts across it and does not react at all to 

earlier formed structural in homogeneities (see Fig. 11.33). More detailed 

analysis shows that the old fractures "revive" if they coincide with the
direction of the principal normal stresses and are generally nor reactivated 

if their location deviates substantially from the orientation of the young 

maximum tangential stresses. It must be stressed that the young fracturing 

(with unfavorable orientation of earlier formed in homogeneities) is not 

sensitive even to rather large ancient faults, in particular to overthrusts 

along bedding (see Fig. 11.33) .

At some observation points young and older fractures were studied 

separately. A sharp difference in the old stress fields from the young was 

observed (even in the case of reactivation of movement on old directions),

which indicates fundamental reorganization of the structural plan in the 

neotectonic stage of development and a change in the mechanism of deformation 

of the crust.

Reconstruction of the stress field on the basis of data of neotectonic 

fracturing at some points was accompanied by dynamic microstructural analysis 

of oriented samples, and also by study of thin sections from drill cores. In 

the vast majority of cases, the old stress fields could be reconstructed using 

such analysis. Data on twinned carbonates (including those from individual 

veinlets) and in some cases in plagioclase made it possible to reconstruct the 

young stress field.

As a result of the investigations, not only could the regional stress 

field be reconstructed for the Pechenga structure, but also local stress 

fields corresponding to tectonodynamic systems of three ranks. The third-rank 

stress field, the shallowest one forming the upper tectonophysical layer, is 

characterized by vertically oriented compressive axes and subhorizontal 

orientation of the other two axes. The deeper second tectonophysical layer 

has a subvertical orientation of relative tension. The deepest layer is 

characterized by a strike-slip field of tectonic stresses and corresponds to 

the region of action of a tectonodynamic system of first rank.

The results obtained made it possible to construct a tectonophysical model 

of the area of SD-3 (Fig. 11.34).

In the Lower Proterozoic deposits, stress fields of three ranks were 

distinguished, differing mainly in size of averaging areas and characterizing 

different depth levels in the crust. Examination of these fields showed that 

a "lens" of less viscous deposits of the Pechenga Complex, differing from the 

enclosing sequence of Archean age in petrophysical properties, was subjected 

to flattening deformation, accompanied by quasi-plastic upward bending of the 

material and its own local stress field, which is characterized by subvertical
Fig. 1I S. 34. Tec t onophy s ical model of the area of the Kola superdeep borehole.

Block diagram. Outcrops of rocks: 1 - Archean, 2 - Lower Proterozoic, 3 - 

marker horizons; orientation of stresses: 4 - relative tension, 5 - intermediate type, 6 - compression; orientation of external forces: 7 - local 

level, 8 - regional level; 9 - direction of movement of deformed material; 

10 - suture faults; 11 - zones of foliation.

Circular diagrams (arrows indicate north). Orientation of stress axes: 12 - 

tension, 13 - compression, 14 - planesof fractures (arcs), directions of scatter in their orientation (arrows), modal orientation of fractures (heavy arcs), 

Diagrams of stress fields: a - Arctic basin, b - regional Pechenga structure, 

c - in Archean part of section, d - for de-stressed zone, e - for upper part 

of section.

197
orientation of the axis of relative distension and more or less uniform 

compression horizontally (see fig. 11.34,d). In this case some increase in 

volume of the deformed sequence should occur. In the upper and lower parts of 

the "lens" of Lower Proterozoic rocks the boundary conditions are acutely 

disturbed, which causes a change in the mechanism of deformation. The sharp 

change in rank of tectonic stress field both on shorter and on longer bases on 

which the reconstruction of the stress state is made, is evidence of this.

The squeezed-out rocks of the middle and lower parts of the section 

described act as a "soft stamp" on the more brittle deposits of the upper part 

of the Lower Proterozoic formations, causing transverse bending in them in a 

vertical direction and an additional local stress field with vertical axis of 

compression and subhorizontal relative tension (see fig. II.34,e). The rank 

analysis of the stress field shows that the boundary between the 

tectonophysical layers would run at depths of the order of 3500-3800 m.

The described mechanism, of formation can really arise only in the' case of 

slippage due to horizontal compression of the base of the deformed "lens" of 

deposits of the Pechanga Complex on the older formations. Actually, the 

construction showed that at the boundary of the Lower Proterozoic and Archean 

deposits (depth on the order of 6800 m) there is a new change in the tectonic 

stress field. This field is of strike-slip character with subhorizontal 

orientation of both the compressional and relative tension axes (fig. II.34,c) 

and indicates displacement of the material layer-wise along the boundary of 

the complexes of different age. It can be expected that at depths of the 

order of 13-15 km a zone of displacement and separation into layers will be 

observed, depicted in the figure and kinematically corresponding to an 

overthrust along the bedding. Petrostructural investigations of the Archean 

deposits from the lower part of the section showed ''the possibility of 

distinguishing two successive (in time) stress fields, one of which 

corresponds to the stage of formation of the schistosity and is characterized 

by a compression axis oriented normal to it. The other, the younger, stress 

field is reoriented so that the plane of schistosity is parallel to the area 

of action of maximum tangential stress, i.e. the idea of displacement of 

material along layering is confirmed by the " ^ ., data.

Analysis of the stress fields of different rank suggests that there is 

clearly expressed horizontal layering of the crust, related not to extensive 

manifestation of horizontal displacements in it, but to a change in local 

conditions and mechanisms of deformation of different deep horizons.
Thus in tectonophysical respects the Pechenga structure is a region of 

pressure characterized by high confining pressure at depth, produced by 

compression and some increase in volume of the rocks in the middle part of the 

section penetrated by the hole. At the base and top of this layer special 

boundary conditions arise, leading to reorientation of the tectonic stress 

field and subhorizontal layering of the crust, which is recorded by 

seismogeologic methods.

Thus on the basis of geophysical investigations of the section of SD-3 and 

systematic measurements of the physical properties on core samples, 

geophysical and petrophysical sections (models) of the structure of the upper 

part of the crust, including seismoacoustic and magneto-electrical (magnetic 

and electrical properties according to measurements in the hole and on 

samples) models, a model of the natural radioactivity of the rocks (from 

logging data and measurements on samples), and an elastic-density model were 

constructed. Analysis of the vertical zoning of physical properties of the 

rocks and crustal structure in the section of SD-3 and the area around it made 

it possible to establish the following:

The seismoacoustic model reflects in detail the distribution of elastic 

wave velocities, modules of elasticity and effective sampling in the section. 

The quality of acoustic logs was markedly lower at a depth of more than 4500 m 

in connection with an increase in cavities in the hole and in its average 

diameter. Below 4500 m a zone of low elastic wave velocities was noted, which 

is traced in the rocks of the Pechenga (to 6842 m) and Kola (to the bottom of 

the hole) complexes. The zone of low velocities stands out relative to the 

upper high-velocity part of the Proterozoic Pechenga complex and primarily 

reflects a sharp drop in elastic wave velocity with depth.
APPENDIX

Conventional symbols for 

_ lithologic columns

Rocks

Proterozoic group 

Phyllites

Siltstones

Sandstones, metamorphosed sandstones

Sandstones, gritstones, conglomerates

Metarn-sandstones, gravelly sandstones, rine-fragmental 

conglomerates

S,andy. lime stones, dolomites, meta- morphosed

Calcite, calcitedolomite, talc-tremolite marbles 

Quartz-mica-carSonate & quartzmica schists, metamorphosed quartzites & sandstones 

Basic tuffs: a = 

Itfpelitic, b = psam- mitic; metamorphosed

Lava-tuff breccia 

and fine basic 

turfs

itoi

B-iotite-amphiboleRiflioSlase schists alter diabases

Melanocratic plagioclaseamphibole rocks

Picrite porptiyrftes

Magnetite-biotite-plagioclase 

schists after andesites with 

intercalations of magnetiteamphibole-plagioclase schists 

after andesites

Magnetite-biotite-plagioclase 

schists after andesites & metamorphosed andesites & trachy- andesites

Serpentinized peridotites, serpentinites, talcsericite rocks

Gabbros

Essexite gabbros

Dacite-andesite 

porphyrites

Achean group

Biotite-plagioclase 

gneisses

Biotite-plagioclase gneisses

with high-alumina minerals

(garnet, staurolite,

lusite, sillimanite)

andaActinplitized lava- breccias., tufr-lavas 

and tuf r-breccias 

Talc-chlorite & 

carbonate-chlorite schists after ultramafic & mafic 

tuffs & effusivee berlcite, sch^scs, metamorphosed 

weathered layer

Diabases, actinolitized diabases - f

Actinolitizecl pillow-lava diabases

PorDhyrgblastic actinolitized

diabases

Magnetite-amphi- box^-plagioclase schists alter 

diabase

er diaoases

Two-mica gneisses, schists 

w. high-alumina minerals

Biotite-amphiboleplagioclase gneisses

Amphibolites

Amphibolites with 

cummingtonite

Metaultramafics and 

biotite-amohibole schists

Porphyritic 

biotite granites

Sulfide impregnation 

Magnetite impregnation 

Zone of cataclasis

200
. DRILLING

Technological and Scientific Basis for 

Choosing of the Drilling Equipment

This section contains the main results of scientific studies of the 

principal problems of superdeep drilling in crystalline rocks with continuous 

coring.

Parameters of Drilling

Theoretical determination of the major parameters of drilling was based 

on the analytical function Tnp = t(hcp l/cno^M) Optimum combination of 

these factors results in minimum time of drilling. 

Tnp " Useful time of drilling

hcp - Average drilled interval during one round trip 

Vcno - Speed of round trip 

Vj^ - Mechanical speed of drilling

Design of the Well

Information on characteristics of rocks adequate for design of the Kola 

well were not available.The technology that permits corrections during 

drilling was applied. Essence of the method was as follows. After permanent 

casing of the drilled interval, a temporary casing that can be withdrawn is 

fixed on the surface. Then the drilling resumes. ' If new casing is required, 

the temporal case is withdrawn and the drill hole is widened.

Stability of Rocks around the Drill Hole

Different components of the stress field have been theoretically 

assessed. Expected behaviour of rocks around the drill hole depending on 

depth and their physical characteristics are shown in Fig. III.5., where 

~~ hydrothermodynamic stability, H - depth.

901
Permissible Parameters of the Spatial Trajectory of the Well

Calculations show very tough requirements to the parameters of inclination 

of the deep wells, especially in their upper intervals. See Figure III.6.

Method and Regimes of Drilling. Prognosis of Indices of the

Wear and Tear of Bits

Calculations showed significant advantages of turbodrilling over rotary

drilling at depths over 10 km. Optimum frequency of rotation appeared to be 

100 to 200 rotations per minute. Thermostable reduction turbodrill has been 

found to be the best bit when temperature exceeds 150°C.

Drilling Device

Calculations have been done to develop light alloys with required 

properties for the drilling pipes. At the top of the pipe string, steel 

piping 1.5 to 2 km long is recommended; then aluminum below this. Analysis 

showed strength requirements for the tool joints.

Drilling Mud

Analysis of the drilling conditions revealed certain advantages of 

drilling and with coarser clay particles; kaolinite rather than bentonite 

should be the base for the drilling mud.

Coring

Sticking of core in the core holder is the major problem of successful 

coring, especially in fractured rocks. Technological requirements for the 

coring tool that can decrease sticking are discussed.
Control of Technological Parameters of the Drilling Process

It is nror)osed that bottom well information be obtained 

by a hydraulic telemetric system.

Drilling Rig

Hoisting capacity of the drilling rig must be not less than 4000 kH. 

For casing of crystalline rocks at great depths ^specially designed (using 

foreign models), built-in, round trip mechanism of large hoisting capacity can 

be used. Required characteristics of the pump are: Hydraulic power 930-1100 

kilowatts, maximum pressure of supercharging 35-40 MPa. These and other 

technological requirements were considered during design of the rig 

"Uralmash-15000."/4 three-step system can provide adequate cleaning of the 

drilling mud.

203
SURFACE DRILLING EQUIPMENT AND SERVICES

Drilling Equipment and Electric Drive

To depth of 7,000 m the well has to be drilled by the rig "Uralmash-4E" 

and deeper by the rig "Uralmash-15000."

Controlling System for Technological Purposes

The controlling system consists of several subsystems: Control of 

mechanical drilling, round trip, and flush, and control of the main parts of 

the drilling equipment.

Services

Services on the well consist of two complexes: One to service major 

operations for drilling and logging and another to support organization of the 

drilling process. The first is located on the platform of the rig and adjoining 

building. The second includes repairing shops, warehouses, 

stores for core, etc.

204
,, years years

0,1 Q,5

Figure III.l. Dependence of Tnp 

on basic parameters.

Figure III.2. Dependence on Tnp on 

Hcp if VM = 2.5 meter/hour.

<J', no *J.aJJ0.30,73.53.S \0.<f (JJ 3.2 9.1 M.,

Figure III.3. Graph for choosing of basic parameters with Tnp = 5 years

205
Stress, mpa

JO SO 90 120 150 180 2W

Fisure III.4. Dependence of stress (tfp from depth (H). 1 - Calculation on 

lithostatic load , 2 - Calculation on elastic characteristics of rocks.

Figure III.5. Relationship of stability of rocks around the 

drill hole on H and(p ^

206
10 £,KM

Figure III.6. Dependence of permissible change of the total angle of

inclination (0) from depth of a well. 1, 2, and 3 - depths of 7, 10, and 

11.5 km with T = 300 kH (T - friction between the drilling string and 

walls of the hole). 4,5, and 6 - the same with T = 600kH.

20 50 100 150 200 250 t'C

Figure III.7. Dependence of strength of aluminum p^pes on temperature 

(heating for 100 hours).

207
Figure III.17. Apparatuses on the

stand of the driller

Figure III.18. Room of the controller.

208
Drill Bits

Several types of drill bits shown on the pictures were used during 

drilling with coring. The bit in . Fig. III.21 was specially designed for this 

well, others were modernized. All the bits are used for rotary drilling 

except of ISM-214,3/60T (Fig. III.28) that is designed for turbodrilling with 

coring. Figs. III.30 through III.34 show reamers (to increase the diameter of 

the hole), and Fig. III.35 demonstrates the design of the centralizer.

Equipment for Coring

Three types of coring mechanisms have been specially designed for drilling 

of the superdeep well. Two of them are shown in Figs. III.36 and III.37.

Turbodrilling with coring scientifically approved for the superdeep well 

required a significant amount of research and design work. The main aims were 

to decrease the rotation frequency with maintenance of the high torque 

characteristics, to increase the thermal stability, and improve reliability.

Highly Durable Drill Pipes

Drill pipes made of light alloys.(LBTVK0147) and steel joints (ZLK-178) 

(Fig. III.46) are used for deep and superdeep turbo and rotary drilling. 

Traperziform threads specially developed for the well are used in joints. 

Steel drill pipes (TBVK-140) (Fig. III.47) are used in difficult and 

complicated conditions of drilling.
Drill Muds

Several types of drilling muds were used in the superdeep well. Changes 

in the composition of muds were necessary because of increasing depth of the 

well and rise of temperature.

Telemetric System of Indication of Rotation 

Frequency of Bottomhole Motors

The system was developed in the Kola Exploration Expedition and applied 

from the depth of 9745m. It includes a downhole generator of impulses GIZ.03 

and well head receiving device UNP-1. The most important part of the system 

that requires high reliability is a downhole generator working in conditions 

of high temperatures, high pressure/ chemically active environment,and strong 

vibrations.

Equipment o£the Well Head

The superdeep well was drilled in crystalline rocks and no significant

flow of formation liquids was expected. Thus, the equipment of the well head

i 

was simplified. This equipment permitted drilling of the advancing hole,

reverse ciruclation, turning and change of the string, and differ<tflt auxiliary 

operations.

Assemblage of the Lower Part of the Drill Pipe

Depending on the particular purposes and technical conditions, different 

assemblages of the lower part of th? drill pipe were used. The most important

210
was the requirement for maximum coring and maintenance of the verticality of 

the hole.

Technical Means for Preventive Maintenance

With increasing depth of the bore hole/ the preventive inspection becomes 

more and more complicated. Usual precedures become less effective or useless 

all together. Special technical situations developed that can result in a 

breakdown, including the drill pipe float valve, mechanical and hydraulic

downhole catchers for meta^mechanical and hydraulic disconnectors of the 

drill pipe.

Composite Interpretation of the Technical-Economical Results of Drilling

This section considers the main regularities of the process of drilling 

depending on the bore hole depth. An integral index that changes with 

geological and technical conditions of drilling is applied. Data that . 

characterize the affect of new technology on efficiency of drilling are 

analyzed. Analysis of the drilling process discloses interrelations between 

main indices of drilling and geological conditions, permits the development of 

models of drilling at great depths, and improves technology for further 

drilling of the Kola well and new wells in analogous situations.

Technical-Economical Assessment of the Drilling Process

This section analyses the main indices that reflect efficiency of 

drilling: penetration rate, penetration per run, round trip time, time of 

auxiliary work. Time of penetration changed from 21.7%of total time at
0-2000ra to 3.1% at 10,000-11,500m. Penetration rate varied between 1.3 and 

2.5 ra/hour.

Major Tendencies of Changes of Drilling Indices With Depth

Drillability

Traditional methods of assessment were difficult to apply because the 

penetration rate and penetration per run were deliberately decreased in 

potentially complicated zones. In intervals from 0 to 5000m, the drinability 

worsened with depth and the coefficient of drillability K. decreased from 1 

to 0.46. In Archaen rocks at 6,000-11,000 the coeeficient increased 1.5-2 

times compared with the interval of 0-6,000m probably due to changes in the 

structure of the rocks.

Cavity Formation in the Drill Hole

Logging showed that cavities were formed only during drilling, and they 

hardly grew with time. Destruction of rocks had a brittle character. Another 

important factor is a fractured structure of crystalline rocks widely present 

in the superdeep well along its entire length. The largest cavities formed in 

zones of tectonic contacts between different formations.

Temperature in the Drill Hole

To obtain a real measure of temperature, experimental works were 

carried out during circulation with specially designed autonomous thermometers

212
at depths of 6015, 6275, 6950, and 10909m. The difference in temperatures of

o mud moving up and down does not exceed 40 C; distribution of heat flow with

tAe

depth is linear; equilibrium zone of the temperature gradient in mud column 

/?

was found at 5000m? the time of restoration O f the thermal regime in the well 

is not more than 50 hours.

Variation of performance of bottomhole motors with increasing depth. 

During drilling of the well significant difficulties were met because of fast 

wearing out of bearings in turbines in the first stage of drilling. In the 

second stage, the lower rotation rate increased the time between j»«y!>,«.'*i -f :- 

At greater depths and temperatures (over 140-150 C) however, the rubber and 

glues appeared to be of insufficient quality, and this resulted in short 

working periods of motors before wearing out.

 Wearing of Drill Pipes

Major wearing of drill pipes occurred during round trips. The approach

was developed to calculate wearing of drill pipes depending on total length of

round trips. The results were used to establish succession of checking of

pipes and changing their place in the drill pipe string.

>

' > 

Dynamics of Change of the Resistance Force

Specifics of drilling in crystalline rocks result" in increased resistance 

force measured as increase of excessive loading on the drilling hook and in 

different cross sections of drilling string d.using pulling out of the string 

and the torque durinq rotation. Changes of resistance force with depth has an

213
exponential character close to linear in the upper intervals and with maximum 

increase beginning at 1000m from the bottom of the hole. Cuttings at the 

bottom significantly affect the resistance force.

Wearing of Wire Line

Data on wearing of the wireline are shown in Table III.27.

Core Recovery

Of the 11,500 m total depth of the drill hole, 9325.2 m were drilled for 

core recovery. Total length of recovered core is 3700.1 m, or 40.1 percent of 

the total where core recovery was sought.
Figure III. 21. Drill bit KC-212, 7/60 TKZ (2B-K212. 7/60TKZ

215
PMC. 111.23. 5ypM,ifc«a« 

KC-212.7.80TK3-H (25H-K212.7/60TK3)

216
PNC. 111.24. SypM.ifcNa* ro.iotna 

KC-2J2.7,6«TK3-Hy PMC. IIIJI6. BypM.ikNa* ro.io«»a 

1H-K2H.MT3

PMC. 111.23. Bypt«,ifc«a« 

15H-K2H 60K3

217
PHC. 111.27. 5ypn.ifc«»« 

20H-K2H «OK

P«c,

TO H!-2JS.STK3-rHy

218
p*c 111.30.

4PUl-295.3mS.9TK3

paCUlHpHTCJlfl,' MM ..........

 HaHMCHblUHft AOnyCTHMbJH JHaMCTp paCUJHpSCMOH CKBaJKHHbl, MM

Bucora pacuiHpHTe^s, MM, HC 6<xiee ........

uuapoujeK, MM, HC 6o-iee ......

iri

'

LHaMerp ueHTpavibHoro OTBepciHS, MM

ocesas Harpyaxa, xH 

Macca, xr, HC 6o-iee .....

295,3

215,9

740

1,0

50

300

170

K2

219
(0
, . J2T,

Puc. 111.35. UC-Z»,7CT

221
T, /+«

10

d

0-6..

C. IIU8. Typ6oAOJOTO KTJI4C-195-2H'60-80

I Cfto Q t_A"

&0-8C

TexHHiecxan xapaxTepMCTMKa KTJ14C- 195-2 14/6 0-80

«- MHCJJO ryp^HHHbJX CCKHHA .

O .ZLiHHa CCXUHH, M ...

(Jl^QUiHHa uinHHaejiu, M ...

CS^MHcno cryneHeA rypCHHbi . 

4? B TOM qHCie a oawofi CCKUHH 

\ HHMO cryncHefl nHTbi .. 

* HHWO cpeaHHx onop ..

°/ B TOM MHC.IC:

OaHOH CCXUHH

// B

Kopnyca, MM:

BHytpeHHHH .......

KCpHOnpHCMHMKa, M .....

// HapyxHUH aHaxerp KepHonpHevHoA rpyCu, 

MM:

/? CbCMHOfl ........

A, /f- HecbeMHoA ........

25.92

3

7,955

4,415 (4,922)

315

105

30

11

195

165

25,835

83

105

Continued next page.

222
BHyTp«HHHA aHaMetp KepHonpHeMHOfl rpy- 

<5bi, MM:

/ f ./**-*-"* A-""***/* 2o CbeMHOH ........ 70

........ 86

. 

' /j / > ' ^i- FIpHcoeaHMHTejifaHue

x . , .

K 6ypHJibHUM rpyCaM .... 3-147

K 6ypH,ibHOft ro.iOBKe c 60-MM KBPHOM 3-161

6ypHJibHOft HMOBKC c 80-MM KCPHOM MK150X6X1 :8

Macca KepHonpHCMHoro Typ6oao^ora, KT . . 4450

./c ...... 28-36

MouiHocrb, KBr ........ 84-178

^MacroTa BpauieHHs. OC/MHH ..... 480 600

° KpytJiuiHA MOMCHT Ha Ba-iy, H-M . . . 1450 2380

j Oepenaji jaweMMs, MHa ..... 6.6 10,8

A/

223
IL OJ1

fylF. pMC. HIJ7. cnap«« KJIM-I9S-2H «0

7 - 

gf -

10 -

t/- 

IZ. - 

/lU 2

$1

xapaicrtpMCTHKa KflM- 195-2 14/60

, J>/c ........ 20 _ 40

HonycTHMas Harpyaxa, xH .....!' 160 200

Macrora BpameHHsi, O<S/HHH ...... 60 600

p*3b<5bi:

3.117 

3-161

, MM:

^ CypH.ibHofl ronoBXH ....... 212 214

q ueHTparopa-xa.iHCpaTOpa ..... 212 _ 214

to xopnyca CCXUHH ........ 195

V xepna ........... 60

/*- ZI.1HH3 CHapflja B jlByXCCXUHOHHOM HcnO.lHCHHH. M 18,58 

/3 KepHOBMCCTHWOCTb B flBVXCeXUHOHHOM HC.nO.1HeHHH ' M ............ 15,5

224
rPMC. 111.41. Ilonepc^Hoe ce^e«M« BMNTOBOlu&rfC'

!t____'' '

\ II ,

 ^^^nr i

*, WT.12-

PNC. 111.42. BHHTOVOA 3«6oflnufl JL2-I72M

U

PMC. 111.43. XapaKT«pMCTMca tMHTOHoro 3»6ofl«oro

Atxraje.n H2-172M: 

e: « MacrOTa spameHHa; .V.,^ vom- 

 K. n. a. (npOMWio«?Ha» 

 ofla, pacxoA Q-23 -i'c)

226
r ^

co 

co

*."a

CO CO

" co

^ 8 ^

K> 

OO CD

| to _ »_ _»

to 10

_Cn -4 00

<o to en

J- CO Oi 

~^t IO 4-

fe g 8

' -^J O\

en to

to to 

r f r

o 1 J_ Cn | tj\ 

1 oo '

~ _ Cn Co 

CO <£3 o to 4- 1 £>

<p c 10 o to c £

 1^ *- 

KO <p V1 

' to 

pS."b;*-"« o y to, cn| -

0 CO £

to 

 CO 

IO 1

4- ro

co co 

en cr.

to to

f r to to 

oo oo

 5^ 

3|

CO tv g

coto 

Q O 

rio (5 

^1

 " a

CO »O

tc-

 - IO

en c^

4- 4-

X) K 

= » ° 00

CCKUIlft ~

Typ6o6yp»

ciyneiicA i 

Typ6imu !

P°B ^?x: (j/

Jl^ttiia KOMIIO

IIOBKII, M

Macca KOMIIOIIUbKII. KT

(IcpCHaTUHIIOC

oTiiouieiitie

PacxoA

>MIIAKOCTII, J,'C

MacTota

Ofl/MMH

<pyTmuuA

MOMCIIT, II -M

>\aKciiHn4uI.IM MOIItHUCTI.,

Icpcna.i 

aiMciuiM, 

Mlla

IIJIC.INol O

°f T'l

^

Cr~- 

c /'v/JiCc'^ t'Ci}*'* 

Al( li-S ^

&/,&< 

Ft^-f}^*^

' "i \ £.j£

Ait.-^ stfwi" 

T& 't-'f.it.* o

SL ', * ft

5n o.f'7/ fT1*

)i fO *C/ ^

01 ^ u/ r

n J-tffer 

j^t-**-*

 ^H* p>

V

\

ftv
PMC. 111.48.

L6TVX-M7

Tpyfi* JIETBK-H7 e UMK«MN 3JIK-178:

; 2 Tpyfia; 3 

G, nr,

PMC. I1I.47. BypHJUNa* rpy«a TEBK-HO c MMKOM 3UJK-J78: 

; Mv<J>T3; 2 rpyfia: J imnne.it>

228
622

CL-CI

dOlKBHCHH
oes

t f HJKHH H V XHHTTO«»d»U 

KBHKK)KirOU *J tBMtf tSAUdOX f U(S«OtlHHB5 tXDHr 

in rw

OJOHIM1X* »UMi 

"Will BIT 9^609 « 3 x 

-r
J^w^ey

PMC. 111.57. fIep«flyCKHON

KOJIOMMW

PMC. 111.58. MexiMM««cxN*

"PiK. 111.59. r*xp*i- PMC. 111.60. PasvexMHMTCJib

KOJIOMMM P6K-195

. 

-W

231
Pacxoa

TABJIUUA III.18

aaitepa

revnepary-

\ ^

'}~»s*J() >*>

890

299

3470

4000

4540

4850

6015

6275

6510

6950

,£&£ £ '< 

craTUMec1 K»8

5(911^

34.6

45,1

51,5

58,6

67.4

75.0

93.2

97.5

110.5

1116,6

jimaiin.

. Mccxan

AmautC

^__

82.5"

£0.6*

103.6*

109.5*

iJjMH*

cnyoicHMoA

6yp!MbMOA 

K04OMMU.

ItfM'rtL A^ ^nf >fc,

10600

10 160

10 160

2>2 -EM

32 34 .1 c.

TAB/IIIUA III.19

\

pa TCMneparypu. M

3960

6350

7800

8230

10425

10909

10909

10909

alhr

TeMneparypa, 'C

craTimecxafl

56,8

98,2

123,0

131,0

167.8

181.0

181.0

185,4

HiUvcn n.

jiiHaMiiMCcxa*

43,0*

89,0*

123,0*

161,0*

147,6

146,6

uWw,afrv

UCXMe 42 <1 OCT3HOBKH

10909 10 too

185.4

132.0

150.6 ~

 Tes«nepaTypy jauepH.iH noc.it npon«/*yTOIHUX npoMwaoK (13 20 MHH); pacxoa npoMUBOMHOA XXJKOCTH 34 .1,'C.

^_ PNC. 111.64. Cpa$MK pacnp«A«.ieHH« TCMHCparypw a CT»OJI« CXMJKMHM:

/ CTaTMMecxofl: 2 aHHaMHHecKofi. ycraHoSHauieflc* npH Q-32 .i'c

| PMC. MI.83. SoccTiHOm-iexHe retHnepaTypw

l^f'"'

A

7727

+4

232
. b /«

6ypeMM«,

CpeoiMui

Tlep-IOCTk

no urraxny, 

MHa

MncJio 

peftcoB

Cpeufi 

npoxoaxa

3» P«ftC, M

Cpeuee

BpCMI

, <<

MtcroTt

paiucMiu

06 win

31

(Xiopor, MM

pacHCTMoe

CaJcu bfoj

Ko»<t)- 

(pimu-

«HT

0 1000 

1000 2000 

2000 3000 

3000 4000 

4000 5000 

5000 6000

. 6000 7000 

7000 8000 

8000 9000

9000 10000

P1-80±20

1800

1870

3260

2860

2000

2320

2370

2300

7

11

17

11

24

6

11

3

7,6 

6,3 

4,0 

4,2

8.0

8.1

6,0 

15,0

2,44

3.37

2,62

3.01

2,34

1,91

1.71

3,2

350

300 500 

300 500 

300 500

350 450

350 450

300 400

300

0,31

0.3

0,179

0,179

0.283

0.227

0.227

0.227

0,149

0,082

0,083

0,077

0,163

0,183

0,203

0,262

1

0,55

0,55

0,51

1,09

1,23

1,36

1,76

0 1000

1000 2000

2000 3000

3000 4000

4000 5000

5000 6000

6000 7000

7000 8000

8000 9000

9000 1000

2390

1710

2110

_

2250

2210

2000

1700

2510

2410

12

19

17

 .

10

10

13

10

8

6

7.2

7.5

6

3,6

8.8

8,4

9.6

6,8

8.1

3,06

3,75

5,38

__

2.92

6,94

4.01

5.57

2.99

2.38

500 700

600

500 800

_ .

650

500

500

500

500

600

0.057

0.07

0.065

__

0.060

0.050

0.065

0.07

0.057

CL057

0,068

0,055

0,031

0,032

0,OU

0,078

0,099

0,08

0.094

1

0,82

0,43

0.47

0,65

1,15

1,46

1,18

I,-*

PMC. iil.66.

.

TeMneptrypw B CKBJLXMHC npH npCMMBnax (rjiy6MH» 6015 M): 

/ TewnepaTypa; 2 pacxoa

233
OXHH o«opot 

MOCTX d or r^ydHHu CXJUJKMHU:

-300^.700 <x5./uH«; ^-Harpy,^ 80*20

P*c. 111.42.

234
ia^

0 20<M)

2000 2100

2100-2200

2200 2300

2300-2400

2400-2500

2500-2600

2000 2700

2700-2800

2800 2900

2900-3000

3000-3100

3100-3200

3200 3300

3300-3400

3400 3500

3500-3600

31)00-3700

3700-3800

3MOO-3900

3!KK)- 4000

4000-4100

4100-4200

O(II.VM iKHdwitiiu, M', na )

1M.III 

I'JTti r. 1977 r.

4.11

107!) r.

ILMI

\/QlU>n fi. H> &1J/A0

131 oOl.CM KOJIOIIIIU <7

3.59

4.89

4..7B

5.14

5.2ti

4.82

4.56

5.32

4.52

4.15

4.15

4.18

4.23

4.12

4.09

4.01

4.30

4.57

4.25

11

4.1

3.85 '

4.2<»

5.31

5.1

5.47

5.6

5.18

4.6

5.76

4.50

4.26

4.3

4.30

4.48

4.41

4.34

4.67

4.83

5.1

4.79

4.48

1.45

4.45

4.31

4.87

4.83

5.19

5.24

, 4.87

 4.37

5.39

4.81

4.25

4.25

4.35

4,37

4.29

4.26

4.27

4.S7

4.49

4.56

4.25

4.23

4.14

4.32

5,55

5.04

5.56

5.50

5.3

4.78

6.04

4.99

4.27

4.18

4.43

4.14

4.09

4.17

4.18

4.66

4.57

4.5

4.33

4.11

3.89

Hiirv|>uiJi oftMcp*.

M

7300-7400

7 400 7 T>00

7 500 - 7 (K)0

7 IXMJ 7 700

7 700 7 800

7800-7900

7900-8000

8000 8 100

8 100-8200

8 200 8 300

8 300 8 400

8 400-8 500

8500- 8600

8 600-8 700

8 700-8 800

8800-8900

8 900 9 000

9000 9 KM)

9 KM)- 9 200

9200-9300

9 300 9 400

94 00 -9 fiOO

9500- 9<>00

Vr

;«» Vll 

l!»78 r.

8,90

10,78

10,29

10,03

8,80

W *~* ^J ^ ** s O6*CM CKIUMnUM, M', H4 M* , Jt:

 -'.X 

I!)7M r.

11,74

11,79

9,29

10.28

7,17

0,48

10,23

9,51

7,70

0,08

10,00

30 X 

1978 r.

13,04

13,44

11,22

12,45

8,47

10,9

10,3

9,35

8,49

0,19

10,09

5,01

27.11 

197'J r.

7,88

8,31

12,29

11,85

10,48

10,08

8,08

8,23

10,07

9,2

7,58

0,32

10,15

5,35

5,70

8,37

7,52

IS.VII 

1979 r.

7,90

7,72

9,47

7,72

7,73

8,00

0,85

fi.X 

1979 r.

7,11

9,19

7,40

7,54

8,55

10,84

5111 

l!»80 r.

9,2

8,21

9,21

8,98

9,2

9,73

7,04

to

CO

o>
Table HI. 17 

o>

4200-4300

4300 4400

4400-4500

4500 4000

4000 4700

4700 4800

4800-4900

4900-5000

5000-5100

5100 5200

5200 5300

5300 5400

5400-5500

5500 5000

5000-5700

5700-5800

5800-5900

5900 -0000

00<)0 01 (X)

0100-6200

0200-0300

0300 0400

0400-0500

6500 GOOO

GGOO 0700

0700 0800

0800-0900

6900 -7000

7000 7100

7100-7200

7200 7300

4.13

4.03

4.32

6.50

7.02

4.14

5.00

0,5:*)

5.11

5.39

0.14

0.78

5.02

4,39

4.48

5.09

0.72

7.37

4.98

5,37

0.39

5.19

0.48

4,39

5.18

5.39

4.71

4.87

4.95

8.29

10.81

4.87

7.20

8.19

0.24

0.21

8.70

8.39

5.85

5.10

5.35

0.78

10.40

9.78

0.15

0.97

9.56

7.74

8.91

7.21

7,54

8.81

7.74

0.41

7.54

11.91

9.59

4,'»2

4.04

4.07

7,08

8.38

4.47

5.49

0.82

5.19

5.57

6.03

7.35

6.01

4.75

4.74

5.43

8.74

8.3

5.47

0.02

7.59

6.19

8.03

5.10

5:99

6.67

11.16

10.40

10.57

10.18

10.72

4.05

4,38

4.51

8.37

8.3

4.23

5.87

7.18

5.40

5.02

0.29

7.58

5.09

4.52

4..0

5.31

0.14

9,01

7,04

8.03

12.45

9,28

0 GOO-9 700

9 700 9 800

9 800 9 900

9900 10 000

10000-10 100

10 100-10200

10200 10300

10300 10400

10400-10500

10500 10000

10000 10700

10700-10800

I08W-I0900

10900-11 000

II 000 11 100

II 100-11 200

1 1 200 1 1 300

II 300 11 400

II 400-11 500 . 7

0 *i 

,n.i 
tip

3A71NC

3A7UJ

3A7-fllJlin-2

3A7PT I 11JI1 11-2

3A7ITII!

3A7PTIII-I

4A7PTIII

J12-I72M

A7IIJ PM

A7PTUI PM

JVcft'/'vA'l lliiTC|>ituj 7L'U.I-7I<.0 M /

M|iciKii.\Ha.

M

108,0

--

MllC^I) 

(tcAfllH

' **k

in

-.

_..

IU UAIIII |>VIIC '

ka. u

SV-,

>n

10,5

.__

 .

ro 6y|ifMim.

Tm>e V

peui"rf'j'

4,9

M MilMOIITUUli

tcl^itiv.

 Upf-AA

27.7

_

 -

-_

Infn^*! H"u'|.iiaji 7W»-mi_'H M

M

113,7

308,3

80,8

_

_-

_-.

_.

_.

;r:

15

50

II

_

- 

Mil IMIIII (icflc

"KT

7,0

0,2

7,4

_ .

_.

.._

H|tfMw MC-

''

2 1

2,8

1,7

. _

--

-

...

--

McMtpcHUlltllMA

20,0

21,9

35,1

_..

TvTt-f'i' VI lliiTcjj

rip<ixo.iKa,

M

293,3

48,3

189,7

101,1

171,7

'IncJiu 

pcAcnn

54

7

31

II

17

CO

CO

I'OA

)A7IMC 

IA7U1 

}A7+UlHfl-2

IA7FT+ UIHI1-2

A7rrui

A7ITU1-I

A7PTIII

U-I72M

17111 PM

17PTUI-PM

XK-j^ri/^ lliiTL-piia^ H'JI I-U7II M

-

llp,«».U.. -

41.1

178.0

200.fi

220.<i

29.8

- -

1 1-1,8

'liif/io (iclictiu

7

22

21

22

(i

14

 III! UAIIII (It Ac11 IOXIUK.1

5.9

8.1

9.0

10.0

5.0

8.2

U|>CMM MCXIIIIIIIIIM, M

3.5

2.9

2.7

3.5

2.4

4.2

IIC|lllll.l, M

23.7

33.1

50.8

30.9

13.4

25.7

JK-VKVA^/ iiiiic|iuiji 9711 

II|IIIXOAKM, M

28.7

(W.I

_

_

770.9

MiicJin pclitoii

5

9

_

 .

88

II* 

HpOXUAKa, 

5.7

7.3

_

8.8
^Vjt

t-14

o 

8

_. 

8

X

£

u

To

XCJIOSM

pafioTa.XH-KM

fi H

o t * s

O V O

C * x

°- « t- " «T

O 

55£?£H|

o *» »» 1 O «f

r »''-*

 n

es oo «o oq in CM _ to oo ; to t->. 10 to CM o -«r ; t--. o< to c-« o to ^ o< oo *» 01 o en oo "'''"''"'''

OOOOOOQOOOOO

coc>tootN«O 

 10 c^i t to 

ointNio«ocnioiQ 

OOC-JOOOOCD

04 f*^ to *? co t - 10

 « r^ 10 * Q 

ppTr^^opio

V

C lOQinoiooiooin^^gJ^Q 10 ?? 100 ^^ 1

oooo'oooo'r-"i--ts- r-~ to' to toto»O

<N co co -«r t- «o t- o o co co coi oo oo 001010 T COCNCICS

OO O

ooooo

ooo 

OO 0 00 OO 0 0 0 O

oooooooc5ooo 

)crioc/)-'rcrioC''»< ooooo

,c>

J"> 

 'OOtiJ 

\

F

»O O lO O 1C O l/> O 1C O in cp lO C? lO O IO O 1C CD lO O IO O IO C

r^ 10 CN o r-~ iij c-^ o r-- in o« o t-~ in CN o t~-10 e-» o t--; in CN o r-- ir

10 10 in -T f co co co co CN CN

1F

,__ to -KNO O<N

 <Mcococo-fiOtoto»oioio»o-rTco of CM d «-»

O O O O O O O O O

OC3CDiOOOOiOOiOOiOOOOC5OiO

OOiOOfM OOOI'-OOC't

O O 

OlO

oO 

~ iT^cs o r--iocs o r--IOCNO t--"5<NO t--«O<N o r--"ocso i i i i i i i i i i 

^rlt- h~'t^"to to to*to io*»o"io"io"VV^"Vco"co"co"co'c^<N'cicN" > ' ' ' ' I ' I I '

^

~x^

»- *4

11 Ll
O T ABJ1 llli A 11!.^' 

C8OAHUE AAHHUE nO'PA'CXOJiy ByPHJIbHUX TPyB HA (TEPBOM 3TAHE ByPEHHg Cf-3

AO PJiyBHHU 7263 M

^- -

?

Tf

,

^

^

J

s

i* 

Q

£K£

HcnO.lb3OB3HO Tp>'6

M >^

~\_ T 'C

OT(5paKOB3HO H.IH nepeBeaeHo B

HH3UJ1U"! K.13CC 00 flpHHUHe:

npoBopors B ipyCHOH p«3b6e

M

T

H3HOC3 33MKO8OH pC3b6bJ

M

T

H3HOC3 re-ia II.IH >TaimeHim, M 

/ CpeaHHfi HapsfioTxaiTpyC. pefic 

1 Pacxoa Mera.i.ia KS! 1 M npoXOOXH. KP \ ^.u ^H, 

\ U<c«# ! KtbtJ

.TBT-M7.\II

19025

310

4277

68

14748

242

365 

42,3

oc-T 1 J* si. Mxtfr

C&TTW7^'/3

4314

77

4314

77

150 

32,0

fl.TI»>>-

^/trw'ic/r

1525

25

1525 

108 

52,4

CST

7659'

288.

7959

288

40

/

flpHJieMaHMe. B pacxoi Tpy6 Ha I M npoxojxn HC BK.iK)<4«Hw 4277 M .TBT 

2260 M .1ST I4">. 13 MM H3-3a ya.iori Hapafiorxx M Maccoaoro auxoaa H\ H3 crpoa

npOBOpOTa 33MXOH B TpydHOA p«3b6«.

147X11' MV H 

B p*3y.ibTare

rv 

v

CBOAHUE HAH H WE FIO PACXOHy ByPH^bHbJX TPVB HA BTOPOM 3TAHE 

cr-3.8 HHTEPBA.TE 7263-11500 M

u u A in..1 :

SyPEHHfl

n«.,s,,,w

.:. ._ LoV

HcnO.1b3OB3HO Tp}'<5

M

T

OifipaKosaHO H.III nepeBeicHo B

HH3LUHH sciacc no npHHiiHe:

M

T

JI3HOCO TC.la IUII 33.MK3

M

T

3pO31IOHHOrO pa3MbIBa, M

CpejiHsst HapaCoTKa rpyfi, peflc

Pacxoa rpyfi Ka 1 M^npoxoaKH Kr .' *

-1BTBK-147 

<Ji6T) ' 

LK^vt^" 1 H '

(3>«6T)

19200

306

4922

77

9644

153

4434

291

72

-

.1ETBK-147 

(01953)

L&TvK»/m

( OU?S"3)

15 100

256

15 100

256

367

60

-

flETBK-147 

(AK4-1)

(AX V - 1)

5900

89

_ IM

5900

89

250

20,9

«T C

7700

252

1550

50

6150

202

470

59,3

239
GO CMOOOCiO>OO--O><OIOCM

oooooo

KjK>K3KDKDK3fc)K>

K?OOC/ltA>OO4^K3»v3a>OOOOO

oooooooooooooo

CS3 

^ 

O

OO C*>O)<pK34^-^IOWOlO-4WtOOi -Ol 

O O O O O O O O O O O O O O O O O O 

 K3to<f> 

OCDOO OOOOOCDOOOOO

K3 fO K> »0 fj K> CO CO I

- i O I

, O o i
TABJIHUA 111.27

Hjtma tcaHara, M

tMf^*^ ''^' v»A dx*

JL I'M. . **\

8850

13084

10806

13406

3192

49338

Hirrcpaa* 

6ype«n«, M

ITKTtrvW irt^

7284 8010

8010 9025

9 025 9 993

9993 11059

11059 11514

7284 11514

MHCJIO 

 uaawetiHux

peftcoe

kiLi^LLf-f^

200

219

157

180

36

792

£2v4se-f < wcrjc

yl ^t- - 0 V.

CpeiHva Hapa6orra 

Tueaoro xaHara.

ten -KM

*V'P^

495 620

425 920

487800

490100

516880

489 870

Pacxoa rajeaoro KiHrra. M

Ui^i »V ^re- 1'*^, "^

Ha OAHH peftc

ftr run

44.3

59.7

68,8

74,5

88,7

62,3

na 1 M npo

X01XH J 7

^fcr IM i>> fA+JuT****^

12,2'

13.0"

11,2

12,S

7.00

11,7-..

fej. ar{£

, +.fe~J

t.

0-

k

a

!>

IlHTepsan

HUH, M .

CpejHflH

CTW6HK3, 

HHfl, M .

CT0.16HK3,

HHTepsa.T

HH5J, M . 

CT0.16HK3,

HHTepsa-i

HH5J, M .

CpCJH5JH 

CT0.16HK3,

HHTepaa.i

HUH, M .

CTO.T6HK3,

O o /- / /i_g

6voeJK 0 500 500 1000 1500 2000 2500 3000 3500 4000 6179 

1000 1500 2000 2500 3000 3500 4000 4500 6202

"""CM 13,4 11 17,4 13,1 17,1 13,9 23,9 19,7 17,8 8,9

6ype6202 6300 6403 7233 7324 7410 7508 7637 7706 7813 

' 6300 6403 6411 7299 7410 7508 7558 7647 7809 7902 - ,

JWHH3

CM 6,7 6,6 7,8 5,9 3,9 4,5 3,6 4,9 3,8 4,3

6voe7902 8007 8101 8202 8302 8400 8522 8618 8710 8803 

8003 8101 8190 8302 8400 8494 8589 8701 8803 8901

-3 THH3

CM 8 6,5 2,8 5,2 7,3 6 5 4,5 8,3 8,9

6vpe8901 9003 9103 9202 9303 9404 9510 9610 9902 

9003 9103 9202 9299 9404 9510 9610 9682 10000

" CM 3,7 3,9 4,3 2 1,8 2,7, 2,2 2,5 2,2

6vpe10001 10105 10202 10301 10424 10502 10608 10703 

10105 10202 10301 10350 10502 10508 10703 10750

^"CM 2,5 1,9 2 1.8 1,7 1,9 0,7 0,6

TAB.TIIU A 111.29

/.

I1>rrepa<i.i 6ypemis.

0 1 059

1 059 2 805

2 gQ5 4 673

*. Hrozo:

4 673 5 624

5 642 6 823

6 623 7 263

^ Hroto:

1 263-7 943

8043 9008,4

^ HTOto:

9008.4 10028

10028 10772

10772 11 500

v Kioto:

s- Bcero

Howep 

«olii-j

1 '

2

3

4

HltC.lO

peficoB

> 108

239

265

612

80

125

35

240

39

105

144

104

56

61

221

1*217

npoxoaxa, M 

p Cxrfr^^1 f^j

942

1674

1570

4186

644

865

334.7

1843,7

291,3

742.5

1033,8

835.8

612.2

723.7

2171.7

9235.2

BMHOC xeptta

u

386

913

940

2239

103

260

46.8

409.8

1C:. 8

30S.1

413,9

248.3

163,9

225,2

6374

3700,1

7*

41.0

54.5

59.7

53.4

16.0

30,1

14.0

22

36.3

41,4

40

20

26.8

3L.1

29

4Q.1

C*.***~»-f< ptst~ |

B cpejaeM Sa p«Ac. M

npoxojx*

8.7

7.0

5.9

6,8

8,1

6,9

9,6

7,7

7.5

7.1

7.2

8.0

10.9

11,9

9.8

BfclMOC C,

xepHi

3.6

3,8

3.5

3.7

1,3

2 1

1.3

1,7

2.7

2.9

2,9

2.4

2.9

3.7

2,9

Q

241
TABJIHUA HI .29

Tlovaaareju

vi.W

'

HHOIO peficoB

OfiiuaH npoxoAxa, M

OfilUHH BbJHOC

KepHa

M

%

ripoxoflxa 3a peftc,

M

BbiHoc KepHa 33

peflc, M

/ K.OM-195-2 14/60 £DM-(4r-2/</ /(K

j

' (ipflMas npoMta«xa 

^epea rpynTOMocxy

oj«-

.

ltAu*i

11

75,4

9,84

11

6,83

0,89

xofiyc- 

 yw

vo»t»

>4*pcJ

9

64,8

12,2

18,8

7,2

1,35

UUH<(>OBaiwyn

UMH

*°!cw

5

47

16,7

35,5

9,4

3,34

Odpanui npoMHBxa

Be^fi*- Mrc^iic^r^'

copnyc

IHaMCTpOM 

195 MM,

rpyHTOKOcxa. pacxoj

1 2 Ji/c^

29

238,5

95,25

40

&2

3.3

copnyc

JlUMCTpOM

203 MM,

O^MMHa*

rpynTOHocca, paccoa 6 a ji/c^

8

75,3

39.85

53

9.4

5

E«3 nporpytrroHocxa aanoAueua utaaxoft

v.

^B-^.

39,1

15.9

40.6

6,5

2,65

KTfl<-l9S-2M.'«WO

(^re IjArrt/ m<

\«Ut, O^iiv

PpyHTOMocxa

uenooBMMCMai c 

otfpaiMUM xjianaHOM

^ 

_ 4

^^S2SV3 ,

5.65

20

7,1

1,4

'-2.Mlb>-l<>

/

r

TA5.1HUAin.3i

HHTCpBa.1

6ypeHin, M

7469.4 7943.0

8043,0 8465,8

8506.5 9008,4

9008.4 9344.4

9344.4 9651,0

H T or o

KepM NC nocryna.1 a xaM«py

. B tiHTepBa.ie

Lu L>vT 6f v fr/

<V

19

23

10

26

20

98

H, M

142,4

154,4

71,6

197,3

234,4

799,9

L^. M

45, a

33,4

22.4

34,3

 34.8

170,5

31 p«ftc

par txiK

fS. M

.7,5

6.7

7.2

7,6

11 7

8,2

/, M

2,4

1,5

2,2

1.3

1,7

1,7

BHHOC

32

oo

31

17

15

21

Kepn noctyna.i B «aM«py ~-C&ft

. B iwtepBajJ

U^ uwf txv M

.V

6

10

10

11

4

41

H, -

49,6

72,2

103,9

77 ?

45,6

349,2

V

30.8

57,3

79,5

57,2

23,6

24S.4

33 peftc

h, M

8,3

7,2

10,4

7 1

11,4

8,5

/. M

5,1

5,7

8,0

5,2

5,8

6,1

BUHOC

KepHa,

62

79

77

73

51

71

H B T3<5/:. 111.30.

1<

242
I, O7C'v<M 

IhiTcpuiM 

6ypciiHN, M

Inte-TvA/ /TV,

7469.4 7943

8043 8465,8

8506.5 9008.4

9008,4-9344,4

9314.4 9051

9738-9910 

9918 10028 

10028- 10136

10 136-10 243

10248-10360

10427-10622

10656-10772

10633-10792

10800 11 003

II 003 11 251

II 254-11 499

_

Kii-i9s KA/-IIC* /

U IIIITCpltiMC

A'

1

2

1!

1

1

H, M

5,1

12,6

83,9

9,7

7,3

L^. M

3,2

2,2

27,0

2,65

0,4

_~

.._

--

3« pcflc '

h, M

5,1

6,3

7,0

9,7

7,3

/. M

3,2

1,1

2,5

2,65

0,4

 -

->'

--

__

BUIIOC

Kcpua,

°A

61

17

33

27

5

KAM-I95-2H/00. CKV- HIS/80 '

H iniTcpoa^c 

y i

IK 1* 

A'

II

13

25

4

0

1

4

TiKvM

//, M

99,3

72,-fi

170,2

33,7

47,3

12,7

31,3

_

/...M

29,5

25,8

59,8

2,1

2,2

0

0,0

£tsrttt( 3* pcAc

h, M

7,1

5,6

0,8

8,4

7,9

12,7

7,8

--

/. M

2,1

2,0

2,4

0,5

«,-i

, _

0

0,15

HIJIIOC

Kepnu,

7-

30

35

35

6

5

0

2

MAI'-IOS

^4, j^, /«_. H HIITCplUJIC

l\t -~ £

I*

25

33

20

37

24

8 

22 

12

10

8

14

7

12

12

14

IU

//. M

192

226,4

 175,5

275.2

280

66,9 

104,4 

106,3

100.9

102.7

174,3

82.1

132,2

l'47,2

180.3

185.4

£..-

7C.3

90.7

101.9

91.5

68

3(3.5 

55.8 

26,3

41.6

3 I.ft

39.7

26.7

34,3

37.1

49.2

73

to 

^

CO

(I p H M c q n u H c. N -- MMCJIO peftcoH; // ofinuin npoxoAK.i; i. M HMIIOC xrpiia; /i fpc/iumi ii|>ox<inK.-i 1,1 pt-flo; nwiioc M-piin i;i 

f\J - - a 

c <
.-::* / \

/ /,££££/x

toVBtsaj^ssSS

t- CM «o » >*> <o

/

~* ^' ^3

-> " * f '/< ^\°

:r^^l ;^v-5\

/l,^

\N . ^

X ^>
Figure 1.8. Geological map of the Pechenga region (after Lanev, 

Nalivkina, Rusanov, and Suslova).

Pechenga complex (Lower Proterozoic): 1 - tuffs and 

sedimentary-tuffaceous rocks of different composition and shales; 

2 - volcanites of basite-hyperbasite and hyperbasite composition 

and shales. Southern zone, the Por'itash beds - Shovnyy tectonic 

block: 3 - andesitic, andesite-basaltic metaporphyrites-schists 

and actinolitic amphibolites; 4 - argillaceous tuffites, 

phyllites, siltstones, sandstones and shales; Russel beds - block 

of granite domes 5 - amphibolite and amphibole-plagioclase 

schists with tholeiitic basalts; 6 - varied gneisses and schists 

with argillaceous material in sedimentary and tuffogenicsedimentary rocks. Northern zone, nickel series: 7 - 

metamorphosed tholeiitic basalts (a - diabases, b - metadiabases 

and greenschists, c - amphibolites and amphibole-plagioclase 

schists); 8 - argillaceous phyllites, tuffites, siltstones,

sandstones; Luostarinskiy Series: 9 - metamorphosed

/

trachybasalts. trachyandesites, andesite-basalts (a - 

metadiabases, metaleucodiabases, metaandesites, greenschists, b - 

amphibolites, amphibole-biotite-plagioclase and biotiteplagioclase schists); 10 - metasandstones, metaconglomerates, 

quartzetic-sandstones, dolomites; Tundra series (Lower 

Proterozoic - Upper Archean): 11 - Tal'inskaya suite - micachlorite-actinolite feldspathic and mica-quartz-feldspathic

schists and gneisses, frequently with granite; 12, 13 -

245
Kaskamskaya suite (12 - amphibolites, frequently with granite, 13 

- biotite-gamet-amphibole-feldspathic schists and gneisses) . 

Kola-White Sea complex (Archean), Kola series, upper formation 

14 - biotite-plagioclase gneisses with VGM (a - without 

cordierite, b - with cordierite); middle formation: 15 - 

biotite-plagioclase and amphibole-biotite-plagioclase gneisses 

and migmatites; 16 - biotite-plagioclase gneisses with VGM (a - 

without cordierite, b - with cordierite); 17 - amphibole-biotiteplagioclase gneisses with pyroxene and pyroxene-amphibolites and 

amphibole crystalline schists; 19 - quartz-magnetite schists; 

lower formation (Basement complex): 20 - amphibolites, pyroxeneamphibole-plagioclase schists, gneisses, granite gneisses, 

chainockite and enderbite. Intrusive formations: 21 - andesitedacite (diorites); 22 - diabases and gabbro-diabases; 23 - 

differentiated basite-hyperbasites (a - gabbro-wehrlites, b - 

gabbro-norites); 24 - microcline granites; 25 - microclineplagioclase granites, granodiorites and diorites; 26 - 

plagiogranites and migmatites; 27 - geologic boundaries (a -

complexes, b - formations, series); 28 - principal tectonic

/ 

disturbances; 29 - block diagram section line.

246
Figure I. 80

247
Figure 1.80______ Geologic block diagram of SG-3 drillhole region

Pechenga complex (Lower Proterozoic): 1 - tuffs and 

sedimentary-tuffaceous rocks of different composition and shales; 

volcanites of basite-hyperbasite and hyperbasite composition and 

shales. Southern zone, Por'itash Formation - Shovnyy tectonic 

block: 3 - andesitic, andesite-basaltic, basaltic 

metaporphyrites-schists and actinolitic amphibolites; 4 - 

argillaceous tuffites, phyllites, siltstones, sandstones and 

schists; Russel formation - block of granite domes: 5 - 

amphibolites and amphibole-plagioclase schists with tholeiitic 

basalts; 6 - varied gneisses and argillaceous schists and 

sedimentary and tuffogenic-sedimentary rocks: Northern zone, 

nickel series: 7 - metamorphosed tholeiitic basalts (a - 

diabases, b - metadiabases and greenschists, c - amphibolites and 

amphibolite-plagioclase schists); 8 - argillaceous phyllites,

tuffites, siltstones, and sandstones; Luostarinskaya series: 9 -

i 

metamorphosed trachybasalts, trachyandesites, andesite-basalts (a

- metadiabases, metaleucodiabases, metaandesites, greenschists, b

- amphibolites, amphibole-biotite-plagioclase and biotiteplagioclase schists),; 10 - metasandstones, metaconglomerates, 

quartzitic-sandstones, dolomites; Tundra series (Lower 

Proterozoic-Upper Archean): 11 - Talfinskaya suite - micaceouschlorite-actinolite-feldspathic and micaceous-quartz-feldspathic

scliists and gneisses, frequently with granite; 12, 13 -

248
Kaskamskaya suite (12 - amphibolites, frequently with granite; 13 

- biotite-gamet-amphibole-feldspathic schists and gneisses). 

Kola-White Sea complex (Archean), Kola series, upper formation: 

14 - biotite-plagioclase gneisses with VGM (a - without 

cordierite, b - with cordierite); middle formation: 15 - 

biotite-plagioclase and amphibole-biotite-plagioclase gneisses 

migmatites; 16 - biotite-plagioclase gneisses with aluminiferous 

minerals (a - without cordierite, b - with cordierite); 17 - 

amphibole-biotite-plagioclase crystalline schists; 18 - 

amphibolites and amphibole crystalline schists; 19 - quartzmagnetite schists; lower formation (Basement complex): 20 - 

amphibolites, pyroxene-amphibole-plagioclase schists, gneisses, 

granite gneisses, chamockite, enderbite. Intrusive 

formations: 21 - andesite-dacites (diorites); 22 - diabases and 

gabbro diabases; 23 - differentiated basite-hyperbasites (a - 

gabbro-wehrlites, b - gabbro-norites); 24 - microcline granites;

25 - microcline-plagioclase granites, granodiorites and diorites;

26 - plagiogranites and migmatites; 27 - geologic boundaries (a - 

complexes, b - formations, series ; 28 - principal tectonic

disturbances; 29 - conversion points and'boundaries of divergent

* * > 

waves (PS).

249