Q“

Q...

 

 

This is to certify that the

thesis entitled

A TECTONIC RECONSTRUCTION
OF THE URAL MOUNTAINS, U.S.S.R.

presented by

Jay Brian Silber

has been accepted towards fulfillment
of the requirements for

M.S. Geology

degree in

3% % Majorgrofessor

 

 

 

Date 14 October, 1982

 

0-7639 MS U is an Affirmative Action/Equal Opportunity Institution

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MSU

LIBRARIES
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RETURNING MATERIALS:
Place in book drop to
remove this checkout from
your record. FINES will
be charged if book is
returned after the date
stamped below.

 

 

 

A TECTONIC RECONSTRUCTION
OF THE URAL MOUNTAINS, U.S.S.R.

Jay Brian Silber

A THESIS

Submitted to
Michigan State University
in partial fulfillment of the requirement
for the degree of

MASTER OF SCIENCE

Department of Geology

1982

ABSTRACT
A TECTONIC RECONSTRUCTION
OF THE URAL MOUNTAINS, U.S.S.R.

By

Jay Brian Silber

The southern Urals, central USSR, can be subdivided
into nine elongate north-south striking terranes. From west
to east these are the Ufa-Bashkir, Zilair, Uraltau, Sakmara,
Magnitogorsk, Bredy, East Ural, Turgay, and Ishim terranes.
The first three and the East Ural terrane are composed of
continental crust while the remainder are oceanic in origin.
The Sakmara, Magnitogorsk, and Turgay terranes also preserve
evidence of former island arcs.

The Ural Mountains were created as a result of
obduction of these arcs and intervening back-arc crust onto
the Russian Platform between the Early Devonian and the
Middle Carboniferous. The evolution of the Urals can be
explained solely by westward dipping subduction zones and
without complete closure between the Russian Platform and

the Kazakhstanian plate.

This work is dedicated to Harold and Rhea Silber.

ii

ACKNOWLEDGEMENTS

I would like to thank Kazuya Fujita for his continuous
guidance and helpful suggestions and for the use of his
personal library during the course of this study. I would
also like to thank Drs. Cambray and Trow for their commen-
tary on this manuscript.

Special, thanks go 11) an ‘understanding' office mate,
David Paddock, to April Poelvoorde and to colleagues W. J.
Roger, Jr., M. J. Coley, J. T. Newberry, R. A. Farmer and J.
M. Taylor.

The friendship and intellect of Wayne Schroll have been
invaluable over the course of the past two years.

This study was funded in part by the National Science
Foundation grant 80-25267 and the Petroleum Research Fund

grant G 12366 and is gratefully acknowledged.

iii

TABLE OF CONTENTS

List of Tables............................................ v
List of Figures...........................................vi
Introduction.............................................. 1
Previous Soviet Work...................................... 7
Previous American Work....................................13
Data Sources..............................................15
Identification of Tectonostratigraphic Terranes...........l7
Ufa-Bashkir Terrane.......................................23
Zilair Terrane............................................28
Uraltau Terrane...........................................34
Sakmara Terrane...........................................35
Magnitogorsk Terrane......................................39
Terranes of the East Urals................................42
West Siberian Lowlands....................................45
Kazakhstania Terrane......................................47
Tagil Terrane.............................................53
Polar Urals...............................................56
Paleomagnetics............................................S9
Tectonic Evolution........................................60
Discussion................................................66
Appendix A................................................69
Appendix B................................................95
Bibliography..............................................96

iv

Table
Table
Table
Table
Table

A-I.
A-II.
A-III.
A-IV.
A-V.

LIST OF TABLES

Paleopole positions........................73
Paleomagnetic data file....................79
Paleomagnetic data file....................86
Paleomagnetic pole calculations............92
Data sort routine..........................94

V

Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure
Figure

\l
\DCDQJQONUIubWNt-J
O. O

l—‘H
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12.
l3.
14.
15.
A-l.
A-Z.
A-3.
A-4.
A-5.

LIST OF FIGURES

Location of study area......... ..... ......... 3
Subdivision of the Ural Mountains............ 5
Terranes of the Southern Urals............... 9
Tectonic development of the Sakmara Trough...10
Division of the Southern Urals...............19
Geologic time scale..........................22
Geologic columns of the Southern Urals.......24
Geologic symbols.............................26
Geologic columns of the Southern Urals.......30
Geologic columns of the Southern Urals.......32
Distribution of andesites....................44
Terranes of Kazakhstania.....................49
Seismic profile: Kazakhstania................52
Map of Central and Northern Urals............54
Map of Polar Urals...........................57
Synthesis of reconstruction..................64
Paleomagnetic time scale.....................72

Polar
Polar
Polar
Polar

wandering curve for Kazakhstania.......74
wandering curve for Russia.............75
wandering curve for Siberia............76
wandering curve for three plates.......77

vi

INTRODUCTION

Tectonic reconstructions throughout the world provide
important academic information to scientists and industry.
The Ural Mountains have been a major source of economic
mineral deposits and consequently have received much atten-
tion from Soviet geologists and geophysicists. Little work,
however, has been done by researchers outside the Soviet
Union along the lines cnfaa complete plate tectonic recon-
struction of the Urals: the interaction of the Baltican
(Russian), Siberian, and Kazakhstanian plates and the impli-
cations cflf such interactions. Soviet tectonic reconstruc-
tions use the concepts of vertical tectonics which does not
require the entire region to be treated as a whole, but
rather suffices to explain each structure as an independent
unit with minimal influence imposed by surrounding struc-
tures. Information gleaned from geologic maps and trans-
lated Soviet literature can be interpreted to create a model
where the basic premise is within the realm of currently
accepted geologic and tectonic processes, i.e., the new
global tectonics.

The primary objective of this study is to develop a
plate tectonic model for the origin and evolution of the

Uralian region. In the process, a regional geologic summary

is developed and paleomagnetic data are summarized. A short
digression into the Soviet geologic philosophy is included
in order to better understand their classification of
features and tectonic interpretation. It is not the intent

of this research to study the (Urals in great detail with
respect to every field in the geological sciences, but
rather to create a working model for future researchers to
use as a guide for more detailed studies in their chosen
specialties cu :hi more restricted regions. Although this
study is based on available Soviet data, the data are
approached and interpreted in a context not usually accepted
by Soviet geologists. First, a data base is collected and
discussed, then the Southern Urals are divided into
tectonostratigraphic terranes in a manner similar to Jones
and Silberling (1980). Each terrane is then interpreted in
terms of depositional environments consistent with the new
global tectonics. Divisions of the Urals used by Soviet
researchers have lxuni retained le several instances,
however, additional terranes have also been defined. Using
the information presented, a model is then described,
followed by a discussion of the Viability and advantages of
the proposed plate tectonic model.

The Ural Mountains are located in the Soviet Union
between longitude 55° - 66° 13 and. latitude 48° - 77° N
(Figure 1). This complex orogenic zone ranges from Novaya
Zemlya in the north to the region of the Caspian and Aral

seas in the south. The southern terminus of the Urals is

 

("2'53
0 .

 

~82"! .Moscou
RUSSIAN
(m
PLATFORM
9'“ SIBERIAN

LOWLA DS

 

 

 

Figure 1. Location of study area. Outlines of major
regions are shown. Box outline marks location of
Figure 3. Dotted line is Arctic Circle.

Figure 2. Subdivision of the Ural Mountains (according to
Ivanov et al., 1975).

 

Figure 2.

 

Polar a Cls-Polor Urals

 

64°N

 

Northern Urals

 

5 9°N

 

Middle Urals

 

 

55°N

South Urals

 

 

5|°N

 

Kazakh Urals a Hugodzory Mounrolns

 

 

buried under Cenozoic age sediments. The Ural Mountains are
divided into five segments, the Polar, North, Middle, South,
and Kazakh Urals (Figure 2) by the Russians. This study
concentrates primarily on the Southern Urals and adjacent
portions of Kazakhstania and the Russian and Siberian

platforms (Figure l).

PREVIOUS SOVIET WORK

Horizontal tectonics are not completely unknown in the
Soviet literature; thrusts, thrust faulting, and
allochthonous masses are becoming more widely accepted and
utilized in Soviet geologic interpretations. The use of
overthrusts seems acceptable, although full scale subduction
has appeared in the geologic literature only recently
(Ruzhentsev and Samygin, 1979). The Sakmara region,
Southern Urals (Figure 3), has been reconstructed using
lateral motion of lithospheric "blocks" (Figure 4;
Ruzhentsev et al., 1977), creating a model very similar to
published works on the Appalachians. In comparing the Urals
and Appalachians, Peyve (1973) describes the Polar Urals as
having a very complete geologic section, as does the
northern (Newfoundland) end of the Appalachians. The
southern regions of both mountain chains are less complete.
The ophiolites in both ranges are understood by Peyve (1973)
to be tectonically emplaced; Peyve (1973) further suggests a
global synchronism of principal tectonic stages of crustal
development. The correlation of the Urals and Appalachians
by Peyve (1973) provides details on the Urals and invites
application of a new interpretation to the information
provided.

Ivanov et a1. (1975) describe a model of evolution
which includes many plate tectonic concepts. In their model

the Russian platform, Central Kazakhstania, and the

Figure 3. Terranes of the Southern Urals. For location of
map see Figure 1.

Figure 3.

 

 

I 0'3:
UFA
3:.
BASHKIR
P
RUSSIAN o ‘
PLATFORM “new"
BREDY
URALT U
ZILAIR
+5.2“
MAGNITOGORSK
0
Out
SAKHARA

 

 

 

lO

 

W E
I. Upper Cambrian - Areniq

 

 

2. Arenig - Llandeillo

 

  
  

3. Llandeillo

 

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.’ "
--——--‘---’ "'
‘ .

 

 

 
   
 
 

 

 

 

 

 

 

6. Upper Silurian ---..- -
‘+ “W tfmvw‘uu “‘nnmrmnrutwfido'o“wv‘slx‘ + ‘19-! .
.I u...-.--. ‘ ‘ ‘ A III, I I, ,1 .Q‘O‘....... I
+ A‘AAA _. +
4 A
T Devonian (Eitelian)
EC] Continental crust (East Empm' Alhalic volcanics Arms, qua"; and glaucanite
men
E] Crust d transitimol W m Spilites, 6505““. 5°39." a mm, W! filfitonfiTdfims
- Utramaiic-gabaraic basement [E Andeeites. andeeiric baeam E3 PManitee. eilicic tufts
a My roman oceanic crust EB Dacitee, riparian a Greyuadiee includ‘ng alietaetrornee
m Prata- Uralian oceanic aw E9 Tuttaceaue udrnente [ID Earlier deposits
Figure ’5. Tectonic development of the Sakmara trough. From Ruzhentsev and

Samygi n (I 979). '

ll

Siberian platform represented one large craton during
Vendian to Early Cambrian time. Breakup of the continent
began in the Late Cambrian to Early Ordovician followed by
development of oceanic crust in the intervening rift as
evidenced by extensional features and a parallel (sheeted)
dike complex with an accumulation of tholeiitic basalts and
siliceous slate deposits. Rifting continued. until Early
Silurian time when spreading ceased, subsequent closure of
the ocean. emplaced compressional tectonic structures and
diapiric ultramafics (Ivanov et al., 1975). This
reconstruction obviously indicates a mode of formation for
the obducted ophiolites currently observed in the geologic
record.

Ruzhentsev and Samygin (1979) have also created a model
of evolution for the Uralian region. Their mode of
formation for the Urals is based on compression following
extension that created ea Uralian proto-ocean. This
proto-ocean existed in the Late Riphean with closure
beginning in the Vendian due to the initiation of westward
dipping subduction. Early Ordovician rifting created a
microcontinent which separated the Sakmara region from the
ocean. A Late Ordovician spreading center created basaltic
magmas. Spreading centers continued to exist into the
Silurian with three separate spreading centers being
recognized. Upper Silurian volcanics (spilites and
diabases) were quite common as several central-type

volcanoes existed. Silurian spreading centers continued

12

into the Devonian. Island-arc development. was extensive
during the Devonian as arcs developed in zones this study
has defined as the Magnitogorsk and Bredy terranes (Figure
3). Between these arcs, thoeliites were developed. The

Bredy arc produced extensive calc-alkaline volcanism.

PREVIOUS AMERICAN WORK

World-wide Paleozoic continental reconstructions that
cover the Urals have been published. by various authors
(McElhinny, 1973; Ziegler EN: al., 1977; Morel and Irving,
1978; Scotese et al., 1979; Ziegler, 1981). Hamilton (1970)
dealt expressly with the Urals and associated regions and
this has served as the first order horizontal plate tectonic
model for that part of the world. Since that time, much new
data have been made accessible to the west, filling the
sometimes acknowledged, often present, data gaps and
creating a need for a new analysis. Hamilton's (1970) main
concept involves two continents colliding as an intervening
oceanic plate subducted beneath them. Many of the features
expected in a suture zone (Dewey and Bird, 1970; Ziegler et
al., 1977; Fujita, 1978) are described by Hamilton, however,
many of the processes described are unsubstantiated, i.e.,
using mountain chains with symmetric geology on either side
to infer the presence of a continent-continent collision.

According to Hamilton (1970), the Russian subcontinent
had a stable eastern margin with and island-arc located away
from the continent during the Ordovician and Silurian
periods. Subduction under this arc was dipping away from
the Russian continent; such a geometry would demand the
island-arc to be located on a separate plate. This arc
collided with the continent in Early Devonian time with the

suture zone being the Main Uralian Fault. The

13

14

eugeosynclinal region was elevated and produced sediments
which were deposited in the Devonian foreland basin adjacent
to the Russian platform. A new west-dipping subduction zone
developed oceanward of the accreted arc during the Middle to
Late Devonian to accommodate continental convergence. This
subduction continued until at least Early Permian. Oceanic
sediments were scraped off the crust as subduction continued
and the trench axis stepped oceanward, as did the main belt
of calc-alkaline volcanism.

The Paleozoic of the western margin of Siberia was
primarily a subduction zone with the Russian and Siberian
plates colliding in Permian time.

Ziegler (1981) presents a series of figures which
outline the paleogeographic :movements of continents.
Kazakhstania, Siberia, and Baltica (Russian plate) were
widely separated in the Middle Ordovician. The Middle
Silurian shows the plates coming closer with Laurentia also
in close proximity. By late Early Devonian, Laurentia had
become Laurussia as Laurentia and Baltica sutured.
Kazakhstania joined with the Siberian plate by middle Late
Carboniferous. Early Late Permian shows Kazakhstania (now
sutured to Siberia) colliding with Baltica (now Laurussia).

No suture is shown between Baltica and Siberia.

DATA SOURCES

The data for this thesis are taken from translations of
Soviet literature and maps, consequently it entails the use
of judgement to discern fact from interpretation. Often,
interpretations are given as data based on the assumption
that vertical tectonics control the situation.

Metamorphic rocks are often dated as Precambrian in the
Soviet literature based on their metamorphic grade and the
assumption that intense metamorphism has not taken place in
the Phanerozoic. Radiometric dating has been done by many
individuals and by the Academy of Sciences, U.S.S.R. The
age data given, however, are often K-Ar dates and may not be
consistent with the geology. Thus, care must be taken that
the numbers are compatible with the geology. It must
further be considered that the tectonic movements may create
a situation where overlying rocks are older than the rocks
beneath them.

Ophiolite complexes have been extensively studied in
the past 15-20 years and the Soviets have also made their
contributions to this field. There are some Soviet
geologists who believe ophiolites were once related to the
oceanic crust. Peyve et a1. (1977) describe both ophiolites
and ocean floor as developing over a long time period
accompanied by horizontal movements along various surfaces
within the lithosphere. Others consider ophiolites special

metamorphic formations (Lennykh et al., 1978), while still

15

16

others, not necessarily Russian, suggest they are extrusive
structures that have been rotated 90° to place the sheeted
dike complex in a vertical orientation (Thayer, 1977).
These different interpretations are easily reinterpretable

to provide useful information.

IDENTIFICATION OF TECTONOSTRATIGRAPHIC TERRANES

Soviet subdivision of the Urals is found to correlate,
for the most part, to western concepts of terranes. For
this reason, some Soviet divisions have been utilized in
this study; however, in several cases new terranes have been
defined (i.e., Bredy, Turgay) to isolate regions with
similar tectonostratigraphic evolutions. The Bredy terrane
is the region the Soviet literature usually refers to as the
West Magnitogorsk. Although the Soviets divide the west
lepe of ‘the Urals into :many zones, the east slope is
usually treated as a single zone. In this study we separate
the Soviet East Ural zone into three terranes, the Bredy,
the East Ural, and the Turgay. Nine separate terranes are
identified by this study; a list of these regions, arranged

west to east is as follows (Figures 3 and 5):

a. Ufa-Bashkir terrane

b. Zilar terrane

c. Uraltau terrane

d. Sakmara terrane

e. Magnitogorsk terrane

f. Bredy terrane

g. Terranes of the East Urals
h. Turgay terrane

i. Ishim terrane

l7

18

Figure 5. Division of the Southern Urals. Abbreviation of
terranes: UB - Ufa-Bashkir; Z - Zilair; UT - Uraltau;
S - Sakmara; M - Magnitogorsk; B - Bredy; EU - East
Ural; T - Turgay; IS — Ishim. Other abbreviation: K -
Krak Massif. The Krak Massif is interpreted as being
part of the Sakmara terrane.

 

 

 

 

19
'54- - Jam ‘550 fl
Nyazeetrovslt
Midas
U B
Rueelan ‘
Pla tf arm
52°u 52°N
ls
48° N QBON. "

60°E

 

 

 

 

 

Figure 5 .

20

The Turgay terrane is covered by the same mantle of
sediments as the West Siberian Lowlands but is identified
independently because of its unique subsurface lithology.
The geologic time scale adopted for this study (Figure
6) is taken from time periods used in the
Lithological-Paleogeographical Atlas of the U.S.S.R.
(Vinogradov, 1968, 1969). Absolute dates are from van

Eysinga (1978).

21

Figure 6. Geologic time scale. Breakdown of time periods
used in this study. Absolute dates from van Eysinga
(1978). Periods subdivided into those used by
Vinogradov et a1. (1968, 1969).

22

 

period

 

TRIASSIC

230

 

PERMIAN

zoo

Tatarlon

 

Uiirnian a Kazonion

 

Artl nslrion G Kungurian

 

Asselion 8i Sokrnarian

 

rumpus

345

_l_.; Carboniferous

 

__tA_<Lscovlan

 

Bashklrlan

 

Namurion

#

 

 

r-‘i‘m’aim

 

DEVONIAN

 

 

‘ Famennlan

 

Froenlan

 

Gevitlan

 

Eifelian

 

Early. Devonian

 

SiLURlAN

{m

435

Tiwer

 

Ludiow

 

Wenlock

 

Ll ondoveq

 

PALEOZOIC

ORDOVICIAN

500

Late

 

 

Early

 

CAMBR IAN

 

5 70

L ate Cambrian

 

Malian

 

. Arnginian

 

Lenhn

 

Aldonion

 

PRECAMBRIAN

 

 

____Vo_e_<.l.l_en
Late Riphean
Middle Riphean

 

 

 

gorl! Riphean

 

Figure 6.

 

UFA-BASHK IR TERRANE

The Ufa region (Figures 3 enul 5) is semi-circular in
shape, whereas most uralian structures are linear. It is
bounded on the east by the Bashkir terrane (Figures 3 and 5)
and to the west by the Russian platform. The Bashkir
terrane» extends ‘under' the Cenozoic cover' of the .Russian
platform. Data from a drill hole located 12 km southwest of
Nyazepetrovsk (Figure 5) shows the geologic column
consisting of limestone and dolomite capped by a fbrmation
of sandstone, limestone, and shale with a basal conglomerate
(Figure 7). Paleontologic ages of these rocks show a
complete section of Upper Devonian to Upper Bashkirian (C2)
(Figure 6) rocks. Underlying the above rocks, at a depth of
2000 m limestone and dolomite of Visean (C1) through

Frasnian (D age rocks were encountered (Seliverstov et

3)
al., 1971). This lower group of carbonates is similar to
the overlying limestones and dolomites. The two groups are
interpreted to have been part of the same formation that
have subsequently been thrust into their present positions.
Based on these kinds of data Smirnov and Bellavin (1974)
describe this region as a thrust region and delineate three
separate thrust plates: First sheet - Silurian-Devonian
carbonates (as discussed previously). Second sheet - the
Bardym suite, consisting of Ordovician mafic rocks intruded

by serpentinite, pyroxene and gabbro. These rocks are

overlain by Late Ordovician-Silurian siliceous shale. This

23

24

 

Figure 7. Geologic columns of the

Southern Urals.

25

Figure 7. (cont'd)

 

26

 

 

acid volcanics

andesite

basic volcanics

basic spilite kerataphyre

pebble a: gravel

 

INIEIIIEIEIWI

sand
shale
III-II ,
g: limestone
-l—
li-l dolomite

siliceous rock

a .:
u. n.:’.0:¢'
' ‘ 1“
:.‘ d:—
2.13.}
[153:
. .‘o -
. .e‘-:.‘
‘|:eo a.

red bed

 

 

 

Figure 7a. Geologic symbols.

27

suite has several exposed gabbro bodies, the contacts of

which. dip toward the center' with. depth. Third sheet -
Ordovician rocks in.aa gently dipping thrust over Devonian
rocks. A geologic description of these rocks is not found
in the Soviet literature. The direction of thrusting is
east to west (Smirnov and Bellavin, 1974). This sequence
may be interpreted as an initially passive margin where
oceanic crust has been thrust onto platform carbonates, due

to compressive forces, sometime after carbonate deposition.

ZILAIR TERRANE

The Zilair terrane, in the Southern Urals, is located
to the east of the Bashkir region and to the west of the
Uraltau terrane (Figure 3). The northern terminus of this
zone is at the Krak massif (Figure 5). The geologic column
for the Zilair terrane (Figure 7 and 8) shows a Riphean to
Vendian sandstone and shale complex. Middle Ordovician
sandstone and shale is separated from the Vendian rocks by
an uncomformity (Vinogradov, 1968, 1969; Kamaletdinov,
1961). An uncomformity between the Vendian and Middle
Ordovician rocks appears as the most reasonable solution.

Devonian limestone (about 200 m) is overlain by the
Zilair slate/shale of Famennian (D3) to Tournasian (C1) age,
which has a maximum thickness of 400 m (Khat'yanov, 1976).
Sediment transport was east to west during the Famennian
(D3) deposition of the Zilair formation, yielding sandstone
in the east and siltstone in the west (Smirnov and Smirnova,
1960). Stratigraphically above the Zilair formation is
Carboniferous flysch and Early Permian molasse
(Kamaletdinov, 1961). 1k) Precambrian crystalline basement
is evidenced in the Soviet literature for this region.
Kamaletdinov (1961) lists a metamorphic schist, Cambrian in
age, as the basement for the east side and a period of
erosion or nondeposition for the west. This region, based
on lithology, can be interpreted as a passive continental

margin which is overlain by siliceous sediments of a

28

29

Figure 8. Geologic columns of the Southern Urals. Select
summary columns where adjoining columns represent the
terrane listed as the heading of the left column.
Left column is data taken from the Atlas (Vinogradov,
et al., 1969). Right column provides additional
information, where available from other sources.
Numbers are thickness in meters.

30

600

0.0.0.000
I \/\l\/
J. &

Devonian f f

,\/\/
ff/ VVVVV

1000+ 500+

VVVV

ii I I .
hiatus oceanic

/ \ / \/ crustal
Silurian II II ii I

0.00.00...

basement

/\/\

00.0.0.0...

-—— eooooeooe
VVVVV VVVVVVV
/\/\/ /\/\/

O 0
Ordovician . .7“..—”” v/v v/v\ v/v‘

was

Cambrian ' '

300

Precambrian

 

Figure 8.

31

Figure 9. Geologic columns of the Southern Urals. Symbols
as in Figure 8.

 

3.2

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

Zilar Sakmara Magnitogorsk
Peani
molasse molasse
"9.0.9.06... [Tl—IL ......l....
0 000 000000.. 77.3.”...
coo-ea eeoeee I T I J
I n I ll _ _ _ 1 1
.0000000000 Fl— 4; LI
Carboniterous Luna. 1““. . .2 . .1.“ .r .1. .r
I flysch T. .._.'..':'.'..
— — — \/‘\’J\’
I70 2 0 40
— _ ’ l— — ‘
———.. —’-..‘-.—.:‘.—. e::.-°.°.°.'.::' 2mm
I I or:o¢np\ ’7<‘ ‘7‘ UN"
—— /\l :7. 77.317
:- '—-:‘ ' ' i I Shanda
'p °°fl1 o
I r 1‘ n: L .L
Devonian I I ee 0 e e o co puuSiOSilomF /\ / \ I \
I If
m N, 41+“ ..
3200 2900 4200
1* r _f_[f1_
V.‘ V. ‘14 spilite,
] 1 1 va-v—vv ““5”“ oceanic
T l J 11"}; chart,
SWKMn - -‘fi
.— — — I u u mu
'— Lu— :000000000 Mf
450 800 Tl
— — — b - —
_ 0 0 0 0 0 0 00
oeeeeee e / \ / \
e e e e e e e i-—0 — 0-i
P. {7.73“ \ / \ /
Ordovician L'L'L' ov-v. 7v.
__._. ,/~\,r\/r
6 0 +% 700
meta. 02/ sandstone
schist 9'3 3
C ambrion orgillite
3:73: ..V_ ‘!_V U ultromoiic
T.::::::_“. oooeoooooeoe a
H-.." J L! Viv; gabbro
P'.c°mb'.m b— . - . _ 000.00.00.00

L:

2900

 

 

 

DVVV

800

 

 

 

 

 

 

Figure 9.

 

33

transgressing sea or an inactive marginal basin. A Late
Carboniferous turbidite sequence indicates the final stage

of shallower water continental sedimentation.

URALTAU TERRANE

In the Southern Urals, the Uraltau terrane is located
between the Zilair and Sakmara terranes. The west slope of
the Middle and Northern Urals is often also called the
Uraltau region in the Soviet literature. The terrane is
composed primarily of metamorphic rocks which were
metamorphosed during the obduction of the Sakmara
Ultramafic. These schists have been dated as Lower and
Middle Riphean (Alekseyev, 1976), however this age is
probably assigned on the basis of metamorphic grade, rather
than by analysis of regional geology. The rocks to the east
are part of the Sakmara terrane, but to the west of the
Uraltau schists are Silurian age rocks in conformable
contact, indicating the Precambrian age is erroneous.

The Uraltau terrane was the eastern-most edge of the
passive margin of the Russian platform. The terrane
originated by the horizontal stresses of the subduction
located to the east. This stress is evidenced. by the
predominantly metamorphic rocks: quartzite, schist, gneiss,
eclogite, and marble all of which are folded into large

scale folds.

34

SAKMARA TE RRANE

The Sakmara zone (Figure 3) is usually included as the
western edge of the Magnitogorsk megasynclinorium, but is
here treated as a separate unit because of its unique
geologic makeup and tectonic mode of formation. It is
generally agreed the northern part of the Sakmara zone is 20
to 30 km.‘wide, with the southern. portion increasing in
width. Length of the Sakmara terrane ranges from 200 km
(Ruzhentsev, 1972) ix) 400 km (Kamaletdinov and Kazantseva,
1978). The southern terminus is located just south of the
city of Orsk (Figure 3); it is the northern boundary that is
disputed. According to Ruzhentsev (1972) the Sakmara zone
ends at Beloretsk (Figure 3), but Kamaletdinov and
Kazantseva (1978) suggest it continues to parallel the
Magnitogorsk terrane northward to the city of Miass (Figure
5). The Soviet geologic maps (1:1,500,000, 1972;
1:1,250,000, 1965) indicate no such continuation. This
study defines the Sakmara as ending about the region of
Miass, with the southern terminus extending farther south
than either Ruzhenstev (1972) or Kamaletdinov and Kazantseva
(1978) indicate. For this reason, the terrane is about 500
km long. This definition of the Sakmara terrane is employed
since the southern area. is 'most similar to the Sakmara
terrane, and less closely related to surrounding terranes.

Various terminology has been applied to the Sakmara

region which has resulted in confusion. Sakmara zone is a

35

36

general term often used by Russian authors to define a
region that.1un3 no universally accepted boundaries. This
"zone", at some time in history, was covered by water and
therefore is referred to as the Sakmara basin. This study
has utilized three additional terms in an attempt to clarify
the situation with definite boundaries. The Sakmara terrane
is an area designed to fit the definition of the ‘word
terrane (see Figure 5 for boundaries). The Sakmara
allochthon is the discontinuous west arm of the Sakmara
terrane of which the Krak massif is the northern exposure.
The Sakmara ultramafic is the east arm of the Sakmara
terrane (Figure 3).

The geologic column (Figure 8) for the Sakmara region
shows the base to be Cambrian to Early Ordovician subarkosic
sandstones and argillites of the Kidryasovo suite (Pospelov
and Ruzhentsev, 1972) overlying gabbroic and ultramafic
rocks (Khvorova et al., 1975) presumed to be oceanic crust.
Overlying the sandstones and argillites is a
terrigenous-cherty-tuffaceous sequence, now in a vertical
section, originally consisted of Early Ordovician to Early
Silurian mudstones and siltstones of the Kurgan group in the
west and the K05 Istek formation in the east. The Kos Istek
formation is divisible into the Late Ordovician to Early
Silurian Guberlinskii group of tuff, jasper, and acid and
basic volcanics and the overlying tuffaceous sequence of the
K05 Istek group (Khvorova et al., 1975).

The Ordovician rocks are overlain by a Silurian

37

volcanic-cherty complex which is composed of five groups of
rocks: (west to east) the Sakmara group, Khersonkovskii
group, Baiterekskii group, Blyavenskii group, and the
Sugrala group. The Sakmara and Khersonkovskii groups are
primarily limestone, chert, and flysch while the other
groups are chiefly spilite, diabase, chert, and tuff. This
section can be interpreted as an oceanic sedimentary
section.

An olistostromal sequence (Shanda group) dated Early

Devonian to Eifelian (D consists of conglomerate and

2)
sandstone with limestone and chert, and basalt and tuff.
The Shanda group better fits the geologic column if the
strata discussed above form a system of very intricately
folded tectonic plates (Pospelov and Ruzhentsev, 1972).
Kamaletdinov and Kazantseva (1978) have redefined the age of
a Visean (C1) limestone and basic and intermediate volcanic
sequence as Devonian age. These rocks may be interpreted as
an oceanic sequence with the overlying Shanda group
representing a turbidite from a then present shelf edge.
Structurally the Sakmara terrane is a homoclinal thrust
sheet where Zilair suite (D3) graywackes are thrust from the

east over Late Tournasian (C to Early Visean (C

1) 2)
limestones (Kamaletdinov and Kazantseva, 1978). Using
available data these Zilair suite rocks can be correlated to
the Zilair suite in the Magnitogorsk terrane, however, they

no longer lie in proper stratigraphic succession. The

Zilair suite rocks cover large thrust sheets and extrusive

38

and siliceous rocks of the Betrya suite along with
ultramafics that "intrude" the sequence (Smirnov and
Bellavin, 1974). The Betrya suite may be interpreted as an
Ophiolite sequence. The ‘western. boundary of the thrust
sheet is the ultramafic belt that extends from Orsk to
Beloretsk (the Miass-Sakmara deep fault, Figure 5). To the
east the boundary is buried under the Irendyk formation (see
Magnitogorsk section) of' the .Magnitogorsk zone. Levitan
(1978) interprets these andesite-basalt. volcanics as the
result of an island-arc stage during the Late Silurian and

Early Devonian.

MAGNI TOGORSK TERRANE

The Magnitogorsk terrane (Figure 3), South Urals, is
bounded on the west by the Sakmara zone, a region often
considered as part of the Magnitogorsk terrane by some
Soviet authors, but identified as a separate terrane in this
paper. To the west lies the Bredy terrane (Figure 3), a
region usually included as the west side of the Magnitogorsk
region. A separate geologic column has been compiled for
the Bredy zone (Figure 9).

In the Soviet literature the Magnitogorsk terrane is
often referred to as the Magnitogorsk synclinorium or
megasynclinorium. These two terms, by definition, are not
equivalent (see Appendix B) creating confusion about the
size of the region. The Tagil zone (Figure 13), Central
Urals, is often considered a continuation of the
Magnitogorsk zone by some Soviet authors, but Ivanov et al.
(1973) state that Tagil is runzla structural continuation,
but rather a tectonic juxtaposition. Khalevin et a1. (1969)
point out that the Paleozoic section joining the
Magnitogorsk and Tagil terranes does not thicken toward the
center (by deep seismic sounding (DSS) data) as a continuous
syncline should, and further there is not consistent change
in outcrop age.

The geologic column of the Magnitogorsk terrane shows
no rocks older than Early Devonian (Figure 8). These Early

Devonian rocks are basic and basic spilite-keratophyre

39

4O

volcanics extending through the Eifelian (D2) where they are

overlain by Givetian (D limestone and acid and basic

2)
volcanics. The overlying Frasnian (D3) sequence consists of
acid volcanics, pebbles, sand, and shale which is overlain

by Famennian (D sand and shale. This sequence can be

3)
interpreted as an island-arc environment with volcanism
ending in the Frasnian (D3), followed by a coarse clastic
sedimentation grading into shale sedimentation. During the
Tournasian (C1), rejuvenation of volcanism deposited acid
and basic volcanics which grade into Visean (C1)
intermediate and basic volcanics with limestone, Namurian
(C

limestone, Bashkirian (C sand and gravel, and

2) 2)
Moscovian (C2) limestone. These rocks may be interpreted as
more mature volcanics and andesites grading into a platform
sequence of limestones that was interrupted by a clastic
sequence. SmirnOV' and. Smirnova (1960) describe 'the
Magnitogorsk an; containing volcanic sedimentary sequences
of sedimentary rock, tuff, and tuff—breccia alternating with
sheets and flows of silicic , mafic, and intermediate
extrusives. Among these rocks is the Irendyk formation (D2)
that Levitan (1978) interprets as part of as island-arc
stage. The Karamaltash series of the Eifelian (D2)

(Gorokhov et al., 1962) age basaltoid rocks have differentia-
tion products analogous to sodic rhyolites and dacites of

present ocean basins (NaZO/KZO ratio greater than 4 in) 5)

(Ivanov et al., 1975). The Zilar suite is a Famennian (D3)

to Early Tournasian (C1) (Arzhavitina, 1976) volcanic and

41

clastic formation (Prokin and Ogarinov, 1975) which, in the
western Magnitogorsk region (Bredy terrane) becomes 500-1300
m of entirely flyschoid sediments (Arzhavitina, 1976).
Prokin and Ogarinov (1975) describe a Silurian
spilite-diabase sequence (which may correlate to Early
Devonian on the geologic column, Figure 7) which have high
TiO2 content (1.3-1.7%), similar to ocean basalts, have a
large areal extent, are low in pyroclastics and are
associated with siliceous sediments. Such a geologic
description can be interpreted as indicating a deep sea
origin at a spreading center or a marginal basin.

The spatial migration of volcanic belts from west to
east (Prokin and Ogarinov, 1975) is supported by a plot of
andesite locations (Figure 10) in the Paleozoic taken from
the Lithological-Paleogeographical Atlas of the U.S.S.R.
This migration of andesites may be suggestive of the

direction and sequencing of events of the Uralian subduction

complex.

TERRANES OF THE EASTERN URALS

The East Ural zone (Figure 3) is defined by the Soviets
to extend from the Southern to the northermost Urals.
Unlike the west slope, it is seldom broken into subdivisions
by the Soviets. On the basis of geologic evidence presented
in Figure 5, it is apparent that the East Ural zone should
be subdivided into at least three terranes: the Bredy, lying
just east of the Magnitogorsk terrane , the East Ural,
forming the core of the East Ural zone, and the Turgay,
which extends under the sedimentary cover of the West
Siberian Lowlands. Between the Turgay terrane and
Kazakhstania proper, the existence of another terrane, the
Ishim, may be postulated.

The Bredy terrane is separated from the East Ural
terrane by a band of granites and ultramafics while the
Turgay terrane has a lithology distinct from the East Ural
terrane until Tournasian (C1) time (Figures 7 and 9). Data
from the Turgay terrane are sparse and consist mainly of
exposures along rivers and data from drill holes.

The Turgay terrane can be interpreted as having oceanic
crustal basement overlain by Early Devonian basic volcanics.

These rocks are overlain by Givetian (D and younger

2)

clastics and <carbonates 'with. occasional interbedded. acid
volcanics and andesites.

The East Ural terrane has Ludlow (S age basic

2)

volcanics overlain by Tiwer (S2) basic spilite-keratophyre

42

43

volcanics. Volcanism ceased with Eifelian (D2) and Givetian
(D2) basic volcanics; thereafter minor deposition of
andesite volcanics interrupted platform type deposition.
During the Tournasian (C1) the Bredy, East Ural, and Turgay
terranes formed an east-to-west sequence that fined to the
west. Pebbles, sand, and shale cap Bredy terrane volcanics,
with the last volcanics being Namurian (C2) andesites in the
Turgay terrane.

To the east of the Turgay terrane is the Ishim terrane,
completely covered by Mesozoic and Cenozoic sediments, which
has been defined through the existence of Visean and
Namurian (C2) age volcanic deposits. These rocks are
primarily andesites and a graph of the location of them is
included as Figure 10. These andesites were the primary
basis for the definition of the Ishim terrane.

Precambrian rocks exposed in the southernmost portion
of the East Ural terrane have been interpreted as material
rifted from the Russian Platform (Ruzhentsev, 1972).
Comparison of the lithology of these two regions (Figure 7)
show the rocks to be dissimilar and therefore the origin of
the East Ural terrane should not be interpreted as one of

rifting from the Russian Platform.

Figure 10.
Dotted

ere io't

44

 

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Distribution of andesites in time and space.
lines represent boundaries between terranes.

Ordovician
Silurian

Early Devonian
Late Devonian
Carboniferous

 

WEST S IBERIAN LOWLANDS

The West Siberian Lowlands have been well described by
various authors (Tamrazyan, 1971; Kosygin and Parfenov,
1975; Bazanov et al., 1976; Rudkevich, 1976; Meyerhoff,
1980), consequently only selected information will be
discussed. No granitic crystalline basement is reported in
the Soviet geologic literature. The Triassic to Recent
sedimentary mantle that covers the Lowlands is 8-12 km thick
(Kulikov et al., 1972; Bochkarev and Rudkevich, 1975) with
the deepest region being the Yenisey-Khatanga trough
(Kosyginand Parfenov, 1975).

Data from a drill hole near the center of the Lowlands
shows a porphyry and tuff-lava formation, with quartz
stringers, at a depth of 3000 m dated by the comparative
birefringence dispersion method (on plagioclase) as 326 i 6
Ma (Early Carboniferous) (Bochkarev and Pogorelov, 1968).

Seismic reflection and refraction data shows an
intermediate zone exists between the mantle of sediments
covering the Lowlands and the basaltic basement. This zone
varies in thickness from 2 to 4 km and has folds where limbs
dip 2°- 6° (Bochkarev and Rudkevich, 1975). Trofimuk et al.
(1973) suggest the intermediate zone is rm) Us 10 km thick
and contains oil and gas. A seismic profile has been
interpreted by Krylov et al. (1973) suggesting reflecting
boundaries at 4-5 km, 20-23 km and the Moho at 40 km.

Seismic P-wave velocities are: 5.8 km/sec for layer 2, 6.2

45

46

km/sec for layer 3 and 8.0 km/sec below the Moho.

Based on seismic and drill hole data, the West Siberian
Lowlands can be interpreted as a region devoid of a granitic
crust. Mesozoic and Cenozoic sediments fill the region
floored by oceanic crust which exists due to cessation of
subduction, prior to continent-continent collision, in the

Late Paleozoic.

KAZAKHSTANIA TERRANE

Kazakhstania (Figure 1) is presently located east of
the Southern Urals and is composed of several different
structural-stratigraphic units (Figure 11). Koshkin (1969)
divides Kazakhstania into eastern and western sections
separated by the Central Kazakhstan strike-slip fault which
runs northward from the east end of Lake Balkash and is
proposed to be part of a strike-slip fault that extends from
south of India to Northern Siberia. Antonyuk et al. (1977)
provide a 'more practical division. which runs along the
eastern slope of the Kokchetav and Ulutau (Figure 11)
regions creating the Kokchetav block and the Balkash region
(which includes the Karatau region (Figure 11)). This study
further divides the eastern Kokchetav region into the
Kokchetav, Teniz and Ulutau regions (Figure 11).

The Kokchetav and Ulutau regions have granitic crust
which is Riphean in age based on radiometric dates of
.95-l.2 Ga on granite-gneiss zircon and 1.2-1.4 Ga on
metamorphic zircon (Pavlova, 1978). The present crust of
the Kokchetav region is thick (50-55 km) where 35 km of that
thickness is attributed to the basaltic layer (Rozen et al.,
1974; Rozen, 1977) based on deep seismic sounding (DSS)
data. These features are not seen in the Teniz basin,
rather, an intense magnetic anomaly, relatively low gravity
values, thin crustal layer (35 km) and a thin basaltic layer

are observed (Zeylik and Seymuratova, 1974). Based on D88

47

48

Figure 11. Terranes of Kazakhstania. Dashed lines are
inferred boundaries of terranes.

49

 

 

I“a Petiopavlovsk 1 no \no
KOKCHETAV ..
.92; “ [i I I f
V ‘3
j/TENIZ V\;elinograd
{—33% CENTRAL
I
‘i Korogonda
ULU TAU ,) KAZ AKHSTANIA
I
R

 

 

 

Figure 11.

50

data Zeylik and Seymuratova (1974) infer the existence of a
200 km diameter upward bulge in the Moho and Conrad
discontinuities. Soviet authors have interpreted this
region as an uplift, a downwarp and as a meteorite impact
structure, however an alternative interpretation is that the
region lacks continental crust and is therefore a "hole",
currently filled. with. Cenozoic sediments, to the ibasalt
layer.

Ophiolites are found on the west edge of the Ulutau
region and the north and northwest edge of the Kokchetav
region. Abdulin et al. (1974) suggest these ophiolites are
Riphean in age, while surrounding eclogite is dated at 1.35
Ga (no specific method of age dating is provided).
Ophiolites of the Kokchetav region are dated by Rozen (1977)
at 1 Ga. In an alternative model, Zonenshayn (1973)
suggests these ophiolites were emplaced during the closing
of the Uralian suture; coincident with this closure was the
formation of a marginal basin in the area of what is now
Central Kazakhstan. This marginal basin would provide a
source for creation of an ophiolite.

Volcanics of the Ulutau region are rhyolites with high
K20 content suggesting a mature crust, however, effusive
volcanics of this region seldom mature as far as andesites
(Pavlova, 1979). Serpentinite bodies of the Ulutau are
associated with amphibolite and/or greenschist facies
metamorphism and are shattered and foliated where foliation

planes dip 40°- 70° west (Pavlova, 1979). These westward

51

dipping foliations agree with the curvature of the island
arc and transform faults in reconstructions published by
Zonenshayn (1973). Westward dip of the foliations tends to
indicate this region is on the east side of an orogen and
low grade, mostly pressure metamorphism tends to indicate a
compressional zone where, as first suggested by Zonenshayn
(1973) and later supported. by Ziegler' et al. (1977) an
incomplete collision took place creating a noticeable lack
of high-grade metamorphism.

The seismic cross-section depicted in Figure 12 shows a
break in the stratigraphy at the boundary of the Kokchetav
region and the West Siberian Lowlands. This break may be
interpreted as the edge of the Kokchetav craton and the
compacted sediments of the Lowlands. Note the rise in the
Moho discontinuity in the region of PetrOpavlovsk, which
outlines the edge of the continental material.

The suturing of Kazakhstania and the Siberian plate
occurred during the Early to Middle Cambrian. Southwestward
subduction under Kazakhstania is inferred from the volcanic
rocks in the geologic record according to Vinogradov (1968).
Eastern Kazakhstania is outside the main area of this study
but it is in itself an interesting study which should be

conducted.

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52

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TAG I L TE RRANE

The Tagil terrane (Figure 13), often considered part of
the Magnitogorsk megasynclinorium, encompasses most of the
physical relief of the Middle and Northern Urals. The
southern boundary is at the latitude of Sverdlovsk (Figure
13). The western boundary is marked by deep faults and the
east by the Serov-Mauk ultramafic belt. The geology has
been described by Khalevin and Chervanyakovskiy (1970) as
three structural facies zones: the eastern Krasnoural'sk,
the Middle, and the western Kabanka zones. The
Krasnoural'sk zone is an andesite-basalt association dipping
east 70°- 80° and is Ordovician to Llandoverian (82) in age.
The Middle zone is composed of andesite-basalt,
trachyandesite-basalt, tuff-flysch, and volcanic molasse
dipping east 10°- 20° and Wenlockian (82) to Early Devonian
(D1) in age. The Kabanka zone is a.§wmite-bearing region
much like the Krasnoural'sk region with a similar dip. This
eastward dip, also noted by Karetin (1967), can be
interpreted as indicating this region to be to the west of
the axis of the zone of compression. Sokolov et al. (1974)
describe the eastern regions to be thrust over the western
zones. In the central zone of the Tagil, Karetin (1967)
describes spilites (subalkaline basalts) interbedded with
alkaline-poor diabase of Wenlockian (S2) age.

A seismic reflection survey, in the Tagil zone,

interpreted by Sokolov et a1. (1974) shows a velocity

53

54

54° 60' 66‘
64m 64'
West
Siberian
Russian Lowlands
Platform

0 Pomurshiy piut on

 

 

0 ivdel
so. 6 0‘
I
...l
(9
4
l-
0 Ni. Tagil
o Sverdlovsk
_ 60'

Figure 13. Central and Northern Urals. Outline of Tagil
terrane and ultramafic Pomurskiy pluton.

55

section of the Central/Northern Urals at the latitude of
Ivel (Figure 13). The survey line originates in the
Pomurskiy gabbro pluton (Figure 13), listed.cn1 the Soviet
geologic maps as an ultramafic, to the edge of the West
Siberian Lowlands. Ultramafics appear at the base of the
west side of the cross-section with overlying gabbro and
granodiorite. These rocks dip east at about 30°. On the
east side of the cross-section, volcanic and sedimentary
rocks dip eastward. but are heavily faulted. The fault
pattern is similar to the shearing fault pattern observed in
a melange. Sokolov et a1. (1974) suggest the diorite and
quartz-diorite intrusions piercing the gabbro appear to have
been formed later than the rest of the region, as did the

fault pattern located to the east.

POLAR URALS

The Polar Urals (Figure 1, 2, 14), being that section
located north of latitude 64° N, provide a relatively
complete geologic section with the most significant geologic
feature being‘ the Voykar ultramafic massif (Figure 14).
These ultramafics, located between 64° N and 68° N, have a
southeast strike which makes them coincident with the
topographic expression of iflma Urals. Savel'yev and
Savel'yev (1977) describe the massif as being 200 km long
and divisible into three different rock series: (1) Khulga
formation, the westernmost, is composed of garnet-zoisite
amphiboles, (2) Payer formation of ultramafics, gabbro, and
diabase, and (3) Lagorta formation of amphibolite and
tonalite. The massif is described as an isoclinal fold
overturned to the west or as an overthrust to the west
(Lennykh et al., 1978; Bogdanov and Savel'yev, 1979)
indicating that this structure is part of the western side
of a suture zone. The ultramafic-gabbro ophiolite
association of the Voykar zone has been described by Yazeva
(1979) as a large marginal allochthon of ancient oceanic
crust. To the east, the ophiolite association is replaced
by a belt of tonalites, granodiorites and diorites that are
comagmatic with Silurian-Devonian island-arc rocks that cap
the section. A parallel (sheeted) dike complex, often
indicative of ocean floor, is traceable for 150 km and

varies in width from 1 to 3 km. The dikes, 0.5 to 1 m

56

57

BOPE as.

68‘
68’"
° Vorkuto
P d
VOYKAR .Salelrhar
MASS/F
I
Pec.hora
64
av
60' 55.

Figure 14. Map of the Polar Urals. Dotted line represents
the Arctic Circle.

58

thick, are netamorphosed tx> greenschist epidote-actinolite
facies. This metamorphism is attributed to compression at
the time of formation of the oceanic crust (Yazeva, 1979).
Located to the west of the ophiolite are Paleozoic flysch
and pelagic formations crumpled into recumbent folds forming
tectonic sheets (Bogdanov and Savel'yev, 1979). Detritus

from the ophiolite first appears in Visean (C sediments.

1)
Farther to the west lies undeformed Riphean basement and
Paleozoic platform sediments. The west edge of the
ophiolite has high pressure metamorphic rocks, however no
volcanics are seen with the metamorphosed flysch and pelagic
formations. The east contact of the ophiolite has
quartz-tonalite and diorite which have K-Ar dates of 375 Ma
(Middle Devonian). Farther east the diorites are an Upper
Devonian volcanic and tuffogenic formation which Bogdanov
and Savel'yev (1979) classify as an island-arc association.
To the east of the Voykar massif lies the Lesser Urals
structural facies zone, EH1 Ordovician. eugeosyncline,
composed of clastic-volcanogenic and carbonate bodies of
Ordovician, Silurian, and Devonian ages capped by
Carboniferous clastics.

The Polar Urals may be interpreted as representing the
western side of a zone of compression. No zone of collision

is observed, yet the features of the Polar Urals suggest

their origin is due to a subduction complex.

PALEOMAGNETICS

Appendix A lists all paleopole data available in the
sources consulted (see Appendix A). Each paleopole was then
examined to determine if it was consistent with other data
points from the same plate and time period. Inconsistent
poles and poles which could not be unambiguously assigned to
a specific plate were deleted from the data set. Remaining
pole positions were averaged and polar wandering curves were
constructed.

As can be seen in Figures A—2 through A-6, despite the
scatter, the continents did collide and did so within the
time frame suggested by this study's model.

The polar wandering curves plotted in this study can
not be directly compared with those of McElhinny (1973)
because McElhinny used a longer time increment which

necessarily would yield a smoother curve.

59

TECTON IC EVOLUT ION

Figure 15 summarizes the tectonic evolution of the
Uralian region. Paleomagnetic data shows the Russian, the
Siberian, and the then-fragmented Kazakhstanian plates to be
widely separated by oceanic regions during' most of the
Precambrian. Kazakhstania. was formed. during' the Riphean
when the Kokchetav and Ulutau continents collided, forming
the western region of Kazakhstania. An incomplete suture of
these blocks left a region floored by oceanic crust, which
was later filled with sediments (Teniz Basin). During the
Early and Middle Cambrian the Eastern margin of Kazakhstania
collided with the Siberian plate. This collision signified
the termination of southwestward subduction under the
eastern margin of Kazakhstania. No subduction occurred
along the northern margin of Kazakhstania hence the
Kokchetav region did not collide with the Siberian
continent.

The Bashkir, Zilair, and Uraltau terrane are floored by
granitic continental without intervening oceanic crust. On
this basis it may be concluded that the edge of the Russian
platform extends eastward to the west edge of the Sakmara
terrane. The Sakmara and Magnitogorsk terranes are floored

by oceanic crust. which. was created during the Silurian

6O

61

period and later obducted onto the Rmssian platform. The
driving mechanism for this obduction was a subduction
complex located on the east side of the Sakmara terrane with
subduction dipping westward beneath the Sakmara island-arc.
This short-lived subduction zone created volcanics currently
observed in the Sakmara terrane. Also contributing a
horizontal component of motion was westward subduction under
the Magnitogorsk island-arc. The Sakmara ultramafic was
emplaced in the Late Devonian while the Krak massif and the
rest of the Sakmara allochthon were emplaced during the
final stages of closure of the ocean basin, no later than
Early Carboniferous.

During the Eifelian (D2) a brief period of subduction
created andesite volcanism along the west margin of
Kazakhstania. Also during this time andesite and. basic
volcanics of the Ishim terrane were generated as oceanic
crust subducted eastward under Kazakhstania.

Shortly after the time of closure of the Sakmara
back-arc basin, subduction ceased under the Magnitogorsk arc
and initiated farther east, along the boundary between the
Turgay and .Ishim terranes. This west dipping subduction
continued until Late Visean or Early Namurian time when
subduction ended with final closure of the ocean basin. All
volcanism had ended by the end of the Namurian.

By Late Carboniferous the Zilair terrane was a
terrestrial region with carbonates being deposited between

this terrane and the East Ural volcanic arc. This signifies

62

a post-orogenic environment existed for the western part of
the study area.

Shaley limestone deposition occurred in the Turgay
terrane while sand and shale deposition took place in the
Bashkir terrane. During the Permian period, all orogenic
activity ceased and erosion of elevated land areas

commenced.

63

Figure 15. Synthesis of reconstruction. Cartoons depict
stages of development for the Riphean (R), Cambrian
(C), Early Silurian (S ), Early Devonian (D ), Late
Devonian (D ), Early Cdrboniferous (C ), La e
Carboniferoas (C ) and Permian (P). identification of
terranes is as fallows: R- Russian Platform; UB-
Ufa-Bashkir; Z- Zilair; UT- Uraltau; S- Sakmara; M-
Magnitogorsk; B- Bredy; EU- East Ural; T- Turgay; IS-
Ishim; K- Kazakhstania; SP- Siberian Platform.
Basement identification as follows:

vvvvvv - continental
/\/\/\-'oceanic

 

 

f\/\’

\/ \’\/

VVVVVVVVVVV

vvvvvvvvvv

 

\/’\/\

 

VVVVVV-VVVV
VVVVVVVVVV

64

 

/\’

 

\/\
7j/—__/\ SP 1
\/ \/\/\
"/ \/\/
\/\f‘/\

 

K
\ )———/f___ /\\’/\ \/

 

7/———1

SP

’ \ r \.r’
/\”\f\
\l‘ [\4"

 

VVVVVV /\r\
IV, \
VVVVVV \/\I
I x
\f s’
/\’\
"\.v\

 

 

 

 

R

/\I \/\l
\/\’\/\/
(x/

 

/\’\/\/'
‘\”\./\ It

Figure 15.

 

\"\

 

‘W

 

 

 

 

irl
EU K
1‘, ’\/\/
vvvvvvvv xxvvvvv /\/a\/
(\‘l ’\/\’\
VVVVVVV "/\ VVVV \/\/\/
_

 

VVVVVVVVVVVV

 

 

 

VVVVV

 

 

 

 

Figure 15. (cont'd) 65

03

 

 

 

\‘
RUTS M EU K
‘ /\/\’
/\’\/\ \/\r\

\r \r\/

r\/\’\ VVVVVVV
\l‘f \’

VVV /\’\/
vvvv ""\

 

 

"\/\
I\I\’
\a-‘/\

 

 

 

 

 

’\,\,\ vvvvvvvv Ix"’
" ‘ .—
/>’\n ursu EU T '5 K
\ \’\ .- ’\‘ '/\/\
/\/\/\’\ \/ "\’
,\ e ,\ I
r\\/\ ’\vvvv -~vvvvvvvvvvv 1" \\

 

 

 

'e
~\-

'rl IS

 

I
\ VVVVVVVV

 

 

VVVVVVV

 

 

 

 

’1

_ ‘WSL. I '\i$,\.’, \ ’1
J1 vvvvvvvv \/\’\/ \’

vvvvvvvvvvvv \"‘ " "’

 

 

DISCUSSION

The model proposed here differs from previous studies
in several respects. Unlike Hamilton (1970), we suggest
that Baltica and Siberia never fully collided and that
oceanic crust continued to separate Baltica, Siberia and
.Kazakhstania when relative convergence ceased in the Middle
Carboniferous, a date earlier than suggested by Hamilton.

One of the major differences between this study's model
and the model of Hamilton (1970) lies in the amount and
direction of subduction complexes utilized. This study
suggests only westward dipping subduction with two jumps in
location of the subduction. Hamilton (1970) uses several
subduction complexes with direction of subduction flipping
from east to west or west to east creating geometry that
becomes unnecessarily' complex. In some instances, these
complexities are not confirmed, nor denied, by the observed
geology and in other cases the suggested tectonics are
possible, however a simple model is usually the preferred
explanation. The question. of feasibility‘ is not easily
solved. There is no definitive solution to the evolution of
the Urals, only' a :most. probable :model. This study’ has
proposed a model that is as simple as possible without

omitting information present in the geologic record.

66

67

Additional subduction zones dipping various directions could
be added since there is no evidence for or against their
existence, however such is unsupported conjecture.

The model of Ruzhentsev and Samygin (1979) (see
Previous Soviet Work) suggest subduction originating in
Vendian time. This subduction created .Middle Ordovician
volcanism and Late Ordovician oceanic crustal spreading in
the Sakmara zone. Several of these spreading centers exist
in the model of Ruzhentsev and Samygin (1979) and they are
described as spreading centers similar to those currently
observed at mid—ocean ridges. These spreading centers and
the expansive Sakmara trough are weak points in the model of
Ruzhentsev and Samygin (1979). They have been included
wherever spilites are observed and the size of the large
Sakmara trough/spreading center is a matter of debate since
direct measurements are not available. The amount of
oceanic crustal material generated in the episode of Sakmara
spreading is on the order of that generated in back-arc
spreading rather than the larger scale normally observed in
mid-ocean ridges. The Sakmara trough is required to be
larger in the model of Ruzhentsev and Samygin (1979) to
accommodate the model geometry. This study's model utilizes
back-arc spreading as a mode of formation of oceanic crustal
material, which puts no constraints on the size of the
Sakmara basin.

Termination of activity in the Uralian region is dated

by Ruzhentsev and Samygin (1979) as Late Devonian, an age

68

not supported by the geologic data. It appears their
sequencing is not unreasonable, however the time events
originate and terminate is too early in the geologic record
as evidenced fur the composite stratigraphic columns
presented in this study.

The model presented by this study agrees with the order
of events published by Ziegler (1981), however this study's
model shows Siberia joined with the Russian continent
(Laurussia) by Namurian time rather than Late Permian as
Ziegler (1981) suggests. It is noteworthy that the model
presented by this study fits the geometry of previously
published plate reconstructions, while providing a better
analysis of the timing of events.

The use of translated articles from the Soviet
literature has shown an interesting result in the course of
this study. The model herein described is comparable in
several ways to Soviet reconstructions although it has been
generated without the use of many of the facilities and
information available to the Soviet geologists. This is
significant since it shows that enough of the necessary
information is being translated from the Soviet literature
into English in order that research can be conducted using

translated articles.

APPENDIX A

APPENDIX A

Paleomagnetic Data

Paleomagnetic data collected for this study are
included as Tables A-I, II, III. Data in Table A-II include
all data collected, including data points not actually
included in the final calculations. ‘The information is
arranged in ten columns.

Columns 1, 2, 3, and 4. Location and age of the
samples. Column 1 gives the plate the sample is located on.
Columns 3 and 4 are latitude and longitude. The plate
abbreviations are as follows: R - Russian or Baltican plate,
S - Siberian plate, K - Kazakhstanian plate, U - points
located in the Urals, X - points on the Russian plate
omitted from the final calculation, Z - omitted Siberian
points, Q - omitted Kazakhstanian points. Column 2 is the
time period (1 - 28), Precambrian through Cretaceous, listed
in Figure A-I.

Columns 5 and 6. The declination of the sample is
given in column 5 and the inclination in column 6.

Column 7 is the paleopole as determined by the original
author, listed as northern hemisphere coordinates.

Column 8 gives the number of sites and the number of

samples (site,sample) used for each determination by the

69

70

original author. One or both of these numbers may be
omitted if this information was not available.

Column 9 gives Fisher's circle of confidence 0(95
(2:0.05).

Column 10 is the reference. Those numbers with a /
(i.e., 10/144) are data available in McElhinny, Irving and
the Catalogue of Paleomagnetic Directions and Poles (1972,
1975). References with a ; are taken from the Catalogue and
are not listed by McElhinny or Irving.

Table A-III contains the data in Table A-II sorted by
time period and listed according to plate. Note column 1 is
time period and the plate is not given for each individual
data point. Data listed in this table was used to calculate
the paleopoles of each plate.

Table A-IV is the program used to calculate the average
paleopole for each plate.

Table A-V is the program used to print a sort of the

full paleomagnetic data file.

71

Figure A-I. Paleomagnetic time scale. Absolute ages taken
from van Eysinga (1978). Paleomag index # is the
assigned number used in the paleomagnetic pole program.

72

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

paieamafl
P0'0'd "‘00! t M 0
L 28 ee- 65
Cretaceous M 27 mo
E 26 MI
L 25 l60
Jurassic M 24 .74
E 23 res
L 22 2:2
Triassic M 2i 222
E 20 230
L l9 245
Perm ia n M IS 25:
E I? 280
L I6 290
Carboniferous M 5 ms
E M 345
L l3 360
Devonian M l2 370
E Ii 395
L l0 4:0
Silurian M 09 423
E as 435
L 07 450
Ordovician M 06 475
E 05 500
L 04 SIS
Cambrian M 03 540
E 02 570
Precambrian :f 0' 570+

 

 

Figure A-I.

73

 

 

 

 

 

.oomH embum>aH mHom

.1

 

 

 

 

m.NH m.mn mN

m.NmH n.HN «N

n.5mm m.mH HN

m.oVH o.mm ON

m.mMH 5.0m mH

w.omH m.mv mH

n.55H H.mm 5H

H.HmH H.Hv mH

H.mVH N.m mH
m.mMH w.mv HN H.m m.mv eH
m.mmH w.Nm ON N.mmH m.mN NH
m.mmH m.om mH m.mmH H.Hm NH m.VHN n.Hm mN
m.NmH o.mN NH m.NVH N.vm HH m.m5N m.m> HN
o.SMH N.mm mH m.o> o.OHr 0H m.mmH m.mm 0N
m.meH m.mm mH m.OOH m.mHu m .H.GGH o.mm mH
N.NmH m.ov vH m.va o.NN| n N.vNH m.wm mH
m.va m.mN mH m.QMH m.mHi m h.vnH m.mm NH
H.mmH n.Nm NH m.mom m.Hv m w.mmH m.vm mH
v.m h.mN m m.mom m.vm v m.me m.om mH
m.an m.mm m v.0vm m.om m m.NON m.mm vH
m.hHr m.m m N.hmH m.HN N H.va w.mm MH
m.HHN m.Hm H h.vNH o.NI H m.mmH H.Nv NH

mo 20 mo 20 mo zo
mpsuwmcoq mpsuwumq oEHB oUDUHmCOH opsuHumq mEHB mpspflmcoq mpsuflpmq mEHB
oHom mHom OHom
4HmmDm <HmmmHm «HZ/HBmmvHHwN/wm
.moumHm deflcmumnmemm paw .CMHHoon .cmoHUHum How
vcm.Ni¢ mousmflm CH pouuon mcoHuHmom OHom .mcoHuHmom oHOQOOHmm .Hi< oHoma

74

i00‘

t"?

 

 

Figure A-2. Polar-wandering curve for Kazakhstania.
Polar projection used. Numbers are representative
of time periods as listed in Figure A-l.

00°

75

I00"

90°

 

Figure A-3. Polar-wandering curve for Russia. Symbols
as in Figure A-2.

76

" \4

00

....- +

 

00

Figure A-4. Polar-wandering curve for Siberia.
as in Figure A-2.

Symbols

90°

77

180

270

 

Figure A-S. Polar wandering curves for Kazakhstania,
Russia, and Siberia superimposed.

78

Table A-II. Paleomagnetic data file. Complete file,
unsorted, including all data points gathered.
See Appendix A text for meaning of symbols.

Table A-II.
R 20 59 50
R 19 59 51
R 19 59 51
R 19 59 39
R 05 90 30
R 05 90 30
9 20 99 99
9 20 97 99
9 19 72 102
U 09 97 99
R 09 51 29
R 09 51 29
R 13 59 31
R 13 57 31
R 13 90 33
R 20 49 39
U 20 49 47
U 20 49 52
R 20 53 32
9 20 97 92
9 20 99 114
9 21 71 101
9 21 71 101
S 21 71 101
9 21 75 109
R 19 91 49
R 19 59 51
R 19 53 52
R 19 54 52
R 19 91 45
R 19 57 54
R 19 57 55
R 19 59 55
R 17 49 39
R 19 49 39
R 19 49 39
R 14 59 34
R 14 39 34
x 14 39 34
U 14 54 57
9 14 53 91
9 14 95 90
9 14 53 91
9 14 55 90
9 14 54 92
9 14 34 92
9 14 54 91
9 13 59 93
9 13 55 95
9‘13 59"'93
9 12 39 93

211

117
303
130
42
42
49
222
220

229

219
209

41

243
142
100

103
120
121
102
113

“103

97

-19

-39
-40
41
'35
71

asst;

-12
10
-19

assaéaééééésaasisassésaa

-30
97

23226338

1
392

53.44

52.179
52.179
45.179
42.199
42.199
49.149
95.159
40.150
19.140
21.27

29.49

34.159
31.194
29.159
90.135
57.191
49.159
54.194
90.133
59.114
32.193
35/150
34.149
40.127
49.195
49.199
49.192
45.171
41.172
45.197
44.197
43.199
33.191
39.199
39.179
43.192
37.192
17.127
22.150
49.99

20.153
49.129
41.141
12.159
49.110
49.110
23.154
15.150

”""-29.147 '

24.157

79

.29
.52
.14
.9

.92

.31
.34

.29
.49
.34
.35
.19
.37

.15
.31
.34

.49
.40
.19
.17
.10

10
10
10

2/32
2133
2/33
2/35
2/39
2/39
3/31
3/32
3/55
3/99
3/70
3/71
4/29
4/27
4/29
5/23
5/24
5/25
5/29
5/29
5/29
5/30
5/31
5/32
5/33
5/39
5/39
5/40
5/41
5/42
5/43
5/44
5/45
5/49
5/49
5/49
5/50
5/51
5/52
5/53
5/54
5/55
5/59
5/57
5/59
5/59 A
5/90
5/97
5/99

5/99
5/70

Table A-II.

9 12
9 12
9 12
9 12
9 12

m
.-
H

saasarafifiassaaaeaaa

$83§§§8833382885§=

ccaaaacaxxaaaaamaaaaaaaawmaNNmmmmmcxammcmmm
B 3
89329883293agaaaaagaaaagga33399392333322:989393839

h I‘HM
2833882388388888388236888328222

(cont'd)

104 95
99 59
295 ~59
99 55
99 50
99 53
99 99
311 27
115 4
253 ~27
352 19
1 19
233 51
219 ~23
95 44
91 51
9 ~29
12 12
330 72
123 49
199 19
191 39
42 49
149 51
40 37
212 ~21
222 ~43
229 ~41
215 ~44
227 ~39
233 ~42
230 ~44
231 ~39
294 ~94
223 ~20
219 ~19
213 ~10
217 ~31
207 ~8
212 20
200 ~47
231 ~52
247 ~27
225 ~21
220 ~19
232 ~19
224 ~13
190 11
209 ~30

217

30.149
29.152
23.150
29.193
29.199
32.192
39.154
29.155
29.155
21.152
22.302
37.299
2.344

43.201
22.141
25.193
17.197
35.257
74.19

22.192
4.303

9.129

51.149
19.139
44.179
39.179
45.197
42.195
51.179
42.197
40.199
42.197
40.195
37.155
37.191
41.195
39.174
42.199
50.192
25.199
59.199
49.191
22.190
33.159
34.170
29.155
31.199
29.229
45.199
47.190

80

.29

.97
.47

.22‘

.23
.93

.190
.90

5.91
2.15
2.23
4.44
3.54
2.12
2.33

3.151
3.92

4.219
3.104

10

III-b

21

19
13

ammmu~1¢munmu

5/71
5/72
5/73
5/74
5/75
5/79
5/77
5/79
5/79
5/79
5/90
5/94
5/95
9/90
9/95
7/42
7/59
7/57
9/45
9/55
9/70
9/79
9/77
9/79
9/92
9/111
9/99
9/70
9/71
9172
9/73
9/74
9/75
9/95
9/99
9/97
9/92
9/93
9/94
9/95
9/99
9/99
9/100
9/101
9/102
9/103
9/104
9/109
9/110
9/111

81

Table A-II. (cont'd)

R 14 59 33 220 ~40 41.159 9 9/112

R 14 91 37 229 ~48 49.152 4 8/113

8 14 99 99 294 ~98 39.149 7 9/114

U 14 52 59 250 ~20 20.193 10 9/115

U 14 53 57 257 ~27 19.147 9 9/119

K 29 41 73 19 32 94.192 .13 20 10/53

9 21 59 99 99 59 44.142 19. 9 10/93

9 19 54 97 102 39 9.153 .11 11 10/99

9 19 54 97 109 42 10.159 .7 21 10/100
9 17 54 99 309 ~42 2.137 .13 17 10/103
9 15 54 98 299 ~41 10.149 .20 14 10/119
9 14 54 98 302 ~24 7.314 .12 29 10/117
9 14 51 94 292 ~31 3.190 .41 10 10/119
9 14 54 99 274 ~40 19.192 .9 29 10/121
9 14 54 92 299 ~39 7.159 .19 14 10/122
9 14 54 91 101 72 38.134 7.190 13 10/123
8 13 54 92 295 ~99 25.134 .129 9 10/124
9 13 55 90 299 ~49 9.147 .19 14 10/125
9 11 59 93 94 59 31.154 10/127
9 11 59 93 298 ~47 31.154 10/127
8 11 55 95 125 53 29.199 10/129
9 11 55 95 292 ~42 29.199 10/129
9 07 57 103 194 23 20.300 .133 4 10/131
9 07 59 108 192 10 25.309 .79 9 10/132
9 07 90 119 171 17 21.309 .48 4 10/133
8 08 59 109 159 12 24.311 .20 13 10/134
8 09 90 118 195 14 22.314 .27 4 10/135
9 09 59 109 192 14 23.309 .31 9 10/139
8 09 90 119 199 4 27.314 .20 13 10/137
9 05 57 107 194 ~18 41.309 .22 13 10/138
9 05 57 104 190 ~23 42.311 .19 12 10/139
9 04 54 109 190 2 33.310 .35 12 10/141
9 04 59 109 171 ~8 39.299 .39 7 10/142
9 04 57 107 195 ~17 41.307 .39 9 10/143
9 04 54 102 192 ~13 41.309 .29 8 10/144
9 04 54 105 158 ~3 34.312 17.202 10/145
9 01 59 99 132 24 10.142 .9 14 10/179
9 01 59 99 199 23 17.110 .99 4 10/177
9 01 59 98 190 18 18.119 .25 19 10/178
9 01 59 98 193 9 25.115 .35 11 101179
9 01 59 99 170 22 20.109 .39 10 10/180
9 01 59 98 174 20 20.102 .77 7 10/191
8 01 59 98 179 31 13.99 .24 15 101192
R 01 91 35 344 49 54.240 .29 4 101198
R 01 92 34 348 30 44.231 .57 4 10/199
9 21 42 74 173 ~45 75.273 4. 8 13138

K 19 52 99 225 ~59 54.199 13/43

K 19 52 97 233 ~59 51.180 13/44

9 19 44 70 204 ~49 93.199 13/45

K 15 43 70 204 ~48 93.189 13/55

Table A-II.

K 15
K 15
K 15
K 15
K 14
K 14
K 14
R 01
U 01
9 01
9 01

C:C:C:C:C::Ulllfllflfllnl=2CZ92421::CIBUFUIUIDICIBIC:9=l=imlalliu3flflflflflflflfl4BID|=I.3904”
azaaasssssssassssasssasssaaaaszzsaaaaaa

52
51

293388838828828888883822838838838383888388888288

8883828888383333888883

I

9898893999998388889988398388

(cont'd)

210 ~57
202 ~52
204 ~53
209 ~50
201 ~53
199 ~54
197 ~51
35 39
193 34
339 34

12 12
155 10
193 27
141 90

95.190
95.199
95.193
94.199
97.199
70.209
99.202
49.239
17.224
40.299
37.257
-221122
-131112
’2211‘1
79.199
-381135
-313152
21.157
-341122
’340120
“381128
~19.170
33.137
34.135
42.192
8.141
20.151
7.150
‘199120
19.194
“220132
~19.149

41.210
23.152
34.212
34.132
32.159
47.179
35.191
20.194

9.152
40.179

82

.19

aseags3:3gasa§5§§§§§§§9§§§§9§§§9§§§§

C. “I ”I .I Q. C. ‘0 Q.

‘9fll‘l4fl‘fl4fl Oil-JDJD-hmli#IJIJIJDEDGQKJKJIUIhit)EDIJIJINIGIBIBDFOFOFOIQI¢IQ

‘- QI ”I

Table A-II.

K 13
9 12
2 12
2 12
9 12
9 11
9 11
9 12
9 13

12

12

xxxxxxxanccccxxazaaaxaxaaaaaxaaaaaaaNNm
“
UI

22382388233888388388883939893338388882388883883338
8883'8383888338833883888888888888832228988228888888

(cont'd)

209
294

94
233
290
279

94
101
103

97
301
115
229

40
214
221
225
217
219
241
221
207

40
215
213
224
211
200

42

32
217
223
215
221
192
209
235
190
257
290
210
202
204
209
204
201

199.

197
159
270

-42
-74

93
~49
.57
~55

59

59

57

57
~90

29
-‘g

40
~44
~43
~21
~32
~31

~7
~14

~9

23
~11
~23

5
~5

35
~15
~12

10

~2

15

.5

25
~30

10

11
~27
~74
~57
~52
~53
~50
~49
~53
~54
~51

42
~42

59.193
34.101
50.179
38.203
40.147
29.159
31.154
27.151
21.151
32.192
19.139
‘9'2‘

49.152
41.159
49.194
45.159
33.159
42.197
42.199
20.150
32.199

400‘178

41.193
39.170
44.171
27.197
39.179
21.99

23.171
24.192
29.177
29.157
29.192
39.195
28.209
45.199
19.194
29.229
19.147
49.114
85.190
95.198
95.193
94.199
99.199
97.199
70.209
99.202
-63107
20.192

83

.19
.30

ESIJIVIUIQJ‘d-CI 09-Ibllfllln-IIE;:34I4J hikifll~4¢lflhlfl

anon
NO

11

21
11
10
12

18
11

5:98
5:94
5:97
5:98
5:99
5:103
5:101
:23
5:93
:99
:95
5:102
9:195
9:193
9:194
9:192
9:199
9:219
9:225
9:197
9:222
9:179
9:190
9:191
9:239
9:207
9:209
9:205
9:211
9:220
9:217
9:215
9:219
9:214
9:213
9:209
9:212
9:210
9:199
9:203
9:193
9:194
9:195
9:199
9:197
9:199
9:199
9:200
9:229
9:223

Table A-II.
9 14 55 99
9 15 55 99
9 14 54 91
9 14 59 103
9 14 59 105
R 17 49 39
R 19 49 39
R 19 91 45
R 19 54 52
R 19 59 51
R 19 55 53
R 19 57 54
R 19 54 52
U 19 59 49
R 19 49 52
U 19 57 55
R 19 59 49
U 17 57 55
U 19 53 55
K 17 52 99
K 17 44 70
K 19 52 99
9 19 53 91
9 19 99 99
9 17 54 99
9 19 71 102
R 21 49 39
R 20 49 47
R 20 49 52
R 20 59 51
9 20 53 51
R 21 53 55
R 20 53 55
R 20 53 55
R 20 53 51
9 20 59 92
K 20 49 90
2 20 99 99
9 20 94 112
9 20 94 112
9 20 93 112
9 20 99 91
9 20 70 99
9 20 71 102
9 20 93 107
9 20 59 103
9 21 75 109

(cont'd)
315 ~42
290 ~48
109 71
297 ~95
129 81
40 23
224 ~23
48 39
43 48
49 44
40 37
230 ~37
223 ~39
227 ~27
37 50
227 ~43
227 ~23
224 ~39
39 59
233 ~59
204 ~48
225 ~59
74 88
290 59
159 42
102 94
41 42
49 55
49 42
219 ~45
51 43
77 54
47 70
55 50
41 47
93 80
290 59
290 59
99 93
90 75
103 90
92 71
102 75
102 84
120 93
139 95
297 ~85

“11135
13.149
34.132
53.121
47.125
41.183
39.159
40.190
49.197
43.192
45.173
39.197
44.199
34.170
52.152
45.170
32.172
43.173
91.152
51.190
93.199
54.199
47.151
28.148
-81107
39.183
49.152
52.150
48.153
50.174
43.155
35.159
92.125
45.152
51.194
49.147
25.135
29.149
91.142
52.192
54.145
43.153
53.149
39.183
52.125
53.115
41.199

84

.107

.92

.747
.53
.49
.17
.10

.19
.42
.19
.10
.711
.21
.50
.114
.11
.25

.120
.747
.79

.22

14
10

12
10

11

rao— r-unu- ha
“Om“ OQN

H‘JIQIID"
48 In

UIJIE;ID|UICUCI‘dlfll\JflDID

9:111
9:224
9:204
9:209
9:221
7:204
7:149
7:199
7:199
7:197
7:199
7:190
7:191
7:157
7:194
:34

7:159
7:37

7:195
7.173
7:174
7:172
7:193
7:193
7:190
7:194
9:144
9:149
9:149
9:155
9:141
9:145
9:142
9:139
9:140
9:149
9:159
9:134
9:152
9:153
9:154
9:151
9.150
9:143
9:139
9:137
9:147

85

Table A-III. Paleomagnetic data file. Data sorted by
plate, time period. See Appendix A text for
explanation of columns.

Table A-III.

12
13
14
14
14
15
15
15
15
15
15
15
15
19
19
19
19
19

q

I

17

19
19
19
20
21

3338329333832936823829888286

8888388383882

93

219
209
201
199
197
204
210
202
204

201
199
197
200
210
202
204
209
204
233
204

204
25
225
290
173
19

Kazakhstania
~23 43.201
~42 59.193
~53 97.199
’54 70:2”
~51 99.202
~49 93.199
~57 95.190
~52 95.199
~53 95.193
'50 640188
‘53 67:!“
~54 70.209
~51 99.202
~47 59.198
~57 95.190
‘52 85.1%
~53 95.193
~50 94.199
~49 93.199
~59 51.190
~48 93.199
~59 51.190
~49 93.199
’56 541163
~59 54.199
59 25.135
~45 75.273
32 94.192

86

.22
.9

.40
.44
.40

.70
.40
.50
.70

.55
.299

.23

.21
.13

b)

20

5/50

5:99

13/90
13/91
13/92
13/55
13/55
13/57
13/59
13/59
9:199
9:199
9:200
9/95

9:193
9:194
9:195
9:196
9:157
7.173
7:174
13/44
13/45
13/43
7:172
9:155
13/39
10/53

\

Table A-III.

1 59 95

1 59 92

1 59. 99

1 59 99

1 59 99

1 59 99

1 59 99

1 59 99

1 59 99

1 99 99

1 59 92

1 59 95

1 59 95

1 55 99

2 99 99

3 99 99

3 97 97

3 57 97

4 91 119

4 54 109

4 59 109

4 57 107

4 54 102

4 54 105

4 59 107

4 59 107

4 59 107

5 57 107

5 57 104

9 90 119

9 59 109

9 90 119

9 59 109

9 90 119

9 59 109

7 57 103

7 59 109

7 90 119

9 97 99

9 99 99

10 97 99
10 99 99
11 59 93
11 55 95
11 59 93
11 59 93
11 59 99
11 55 95
11 55 95
11 99 99
55 93

n
h

(cont'd)
Siberia
9 ~29 17.197
12 12 35.257
132 24 10.142
199 23 17.110
190 19 18.119
193 9 25.115
170 22 20.109
174 20 20.102
179 31 13.98
339 34 40.299
12 12 37.257
155 10 ~22.122
199 27 ~18.112
141 90 ~22.141
291 ~47 21.157
317 34 ~39.135
305 34 ~31.152
272 39 ~19.170
1 18 37.299
190 2 33.310
171 -9 39.298
195 ~17 41.307
192 ~13 41.308
159 ~3 34.312 '
197 -7 ~34.122
199 -8 ~34.120
193 ~19 ~39.129
194 ~19 41.309
190 ~23 42.311
352 19 22.302
159 12 24.311
185 14 22.314
192 14 23.309
199 4 27.314
159 14 ~22.132
184 23 20.300
192 10 25.309
171 17 21.309
42 45 41.210
295 ~50 23.152
47 39 34.212
302 ~89 34.132
99 53 32.192
99 99 39.154
91 51 25.193
94 59 31.154
299 ~47 31.154
125 53 29.199
292 ~42 29.189
279 ~55 29.159
94 59 31.154

87

.23
.9
.99
.25
.35
.39
.77
.24
.39
.22
.93
.79
.23
.35
.27
.59
.22
.47
.35
.39
.39
.29
17.202
.43
.52
.19
.22
.19
.97
.20
.27
.31
.20
.33
.133
.79
.49
.19
.53
.21
.19

.39
.500

14

19
11
10

15
19

14
10

11
13
13
12

13

“In.
U

3.05.!)

mm
°m

7159
7157
101179
101177
101179
101179
101190
101191
101192
1:290
1:292
1:277
1:279
1:294
2:94
2:94
2:95
2:91
5184
101141
101142
101143
101144
101145
2:99
2:90
2:91
101139
101139
5190
101134
101135
101139
101137
3:91
101131
101132
101133
4:39
4:40
4:41
4:42
5179
5177
7142
101127
101127
101129
101129
5:103
5:101

Table A-III.

28222833889238383898333933

H h“
88338888288288289238828228888882888838888

(I
3..

33838223822899238232222

97
104

2&5
a;

311
115
290

101

102
113
103
295
299
103
142
100

103
120
121
294
302
292
274

101
270

290

88

(cont‘d)
53 24.157
95 30.149
59 29.152
~59 23.150
55 29.193
50 29.189
27 29.155
4 23.155
~87 40.147
59 27.151
57 32.192
53 23.154
51 15.150
91 29.147
~99 25.134
~49 9.147
57 21.151
97 49.99
50 20.153
79 49.129
70 41.141
45 12.159
94 49.110
94 49.110
'66 392148
~24 7.314
~31 3.190
'40 187162
~39 7.159
72 39.134
~42 20.182
~42 ~1.139
71 34.132
’85 531121
91 47.125
~41 10.149
~49 13.149
~99 40.150
~94 37.155
'92 21137
42 ‘99107
99 47.151
51 19.139
39 9.153
42 10.159
59 29.149
94 39.193
71 49.149
79 95.159
90 90.133

.29

.37
.192

.129
.19
.204

.12
.41

.19
7.190

.14
.107

.91
.20
.19
.399

.13
.19

.92

.11
.7

.747
9.54

4.29
.92

10

29
10
29
14
13

14

5170
5171
5172
5173
5174
5175
5179
5179
5:99
5:23
5:99
5197
5199
5199
101124
101125
5:93
5154
5155
5159
5157
5159
5159
5190
91114
101117
101119
101121
101122
101123
9:223
9:111
9:204
:209
9:221
101119
9:224
3155
9195
101103
7:190
7:193
9179
10199
101100
7:193
7:194
3131
3132
5129

Table A-III.

23823982289

N
on.

71

114

112

89

(cont'd)

59.114
49.147
91.142
52.192
54.145
43.153
53.149
39.193
52.125
53.115
32.193
351150
34.149
40.127
44.142
41.199
22.192
74.19

”QUVNI’D

cbO-‘lfl
O

5129
9:149
9:152
9:153
9:154
9:151
9.150
9:143
9:139
9:137
5130
5131
5132
5133
10193
9:147
9155
9145

Table A-III.

Ulflltltlflliltlhlhshsu-

8%8899922889889999

86$338888898386633383283889339229
888888288888888388888388$88

829288888888829

217

221
224
211

220
232
224
217
219
221

42

217

215
219
209
212
213
217
207

207

215
213

219

(cont'd)
Russia
48 54.240
30 44.231
39 49.239
51 2.344
41 42.199
’35 ‘211fig
~34 33.137
'39 341135
'35 921182
59 21.27
75 29.49
~23 32.159
~12 34.159
10 31.194
~19 29.159
39 43.192
29 37.192
~44 47.190
~40 41.159
~49 49.152
~49 49.152
40 41.159
~44 49.194
~43 45.159
5 27.197
’5 391178
’21 331158
'18 391170
’18 291155
’13 311158
~32 42.187
'31 42.199
~14 32.199
~15 23.171
~12 24.192
10 29.177
~2 29.157
15 29.192
~15 39.199
~9 39.179
’21 381175
'10 391179
'31 421188
~9 50.192
'21 331158
~9 401‘173
~11 39.170
~23 44.171
~9 33.191
~20 37.191
~19 41.195

90

.29
.57
.99

.10
.11
.9

1.9
.9

.19

.13

.20
.39
.25
.42

.71
.17
.45
.49
.45
.20
.49
.79
.49

4.219
3.104

.40
.73
.129
.137

3.151
3.92

‘4 NIUDCI~41OIE;ESJD(IID«Oil-0345

11

990043 Juno

101199
101199
1:257
5195
2139
2139
3:95
3:93
3:94
3170
3171
5:90
4129
4127
4129
5150
5151
91111
91112
91113
9:195
9:193
9:194
9:192
9:207
9:209
91101
91102
91103
91104
9:219
9:225
9:222
9:211
9:220
9:217
9:215
9:219
5149
5149
91111
9192
9193
9194
9:199
9:179
9:191
9:239
5149
9199
9197

Table A-III.

8893883683888832383223333233938333233888386

3828822338388833283368382838333328392832288

219

(cont'd)
23 41.193
23 41.199
57 52.179
~39 521176
~40 45.179
w 4mms
49 49.199
49 49.192
~39 <45.171-
~35 41.172
~44 45.197
~44 44.197
~40 43.189
37 44.179
~43 45.187
~41 42.195
~44 51.179
~39 42.197
~42 40.193
~44 42.197
‘39 901185
~23 39.159
39 40.190
49 49.197
44 43.192
37 45.173
~37 39.197
'39 “1188
50 52.152
’23 321 172
’19 531“
57 90.135
~51 54.194
49 51.149
55 52.150
42 49.153
~45 50.174
43 43.155
70 92.125
50 45.152
47 51.194
42 49.152
54 35.159

91

.424
.424

.49
.34

.19
.37

.15
.31

5.91
2.15
2.23
4.44
3.54
2.12
2.33
.29

.39
.29
.7

.35
.20
.35

.29
.9

.49
.17
.10

.42

.19
.10
.53
.19

5
5

10
15

13

«LONF‘FUN
”it

19

10

15
19

15
11

9:190
7:204
2133
2133
2135
5139
5139
5140
5141
5142
5143
5144
5145
9192
9199
9170
9171
9172
9173
9174
9175
7:149
7:199
7:199
7:197
7:199
7:190
7:191
7:194
7:159
2132
5123
5129
9177
9:149
9:149
9:155
9:141
9:142
9:139
9:140
9:144
9:145

92

Table A-IV. Paleomagnetic pole calculation. Program

20

190
40

90

used to calculate average paleopole positions.

PROGRAM KAZMAG (INPUT. WTPUT. TAPE9)
EGUATIONS TAKEN FROM MCELHINNY. 1973: 24-25.
NPG 19 A TIMEING COUNTER.
INTEGER TIME
REAL INC.LAT.LONG
INTEGER DATA(999.9).NOTIME(29)
PI=3.1415927
PI2=PI/190.
PI3=190.1PI
RENINDB
I=0
I=I+1
READ (9.20) (DATA(I.J).J=1.9)
IF (EOE (9)) 5.30
FORMAT (A1.1X.12.1X.I4.1X.I4.1X.I4.1X.I4)
:ORMAT IS PLATE. TIME. LAT. LONG. DEC. 11C.
PRINT 190
FORMAT (* NHAT PLATE?*)
READ 40. IPLATE
FORMAT‘A1)
NT=0
TIME 8 0
TIME t TIME + 1

C SET EVERYTHING TO ZERO

NPG=0

9XL=0. 5 9XM=0. 0 9XN=0.

9PL=0. 5 SPM=0. 4 9PN80.
PI=3.1415927

DO 90 I=1.N

IF (DATA1I.1).NE.IPLATE) GO TO 90
IF (DATA(I.2) .NE. TIME) GO TO 90
NPG = NPG + 1

DEC=FLOAT(DATA(I.5))
INC=FLOAT(DATA(I.9))

CALCULATE AUERAGE DEC AND INC. .
SXL=9XL+(COS1DEC*P12)*COS(INC*P12))
9XM=9XM+(9IN(DEC*P121*CO9(INCOPIZ)1
98N=9XN+SIN<INC*PI2)

LONG t FLOAT(DATA(I.4))

LAT ' FLOAT(DATA(I.3))

CALCULATE AVERAGE LOCATION.
9PM=9PM+191N(LONO*P12)*COS(LATiPIZ)1
SPL=SPL+1COS(LONG*P12)*COS(LATiPIZ)1
9PN89PN+91N1LAT§PIZ1

93

90 CONTINUE
IF (NPG.NE.0) GO TO 75
NT=NT + 1
NOTIME(NT)=TIME
GO TO 150
75 XR = SGRT((SXL"2) 4' (SXM‘H‘Z) + (SXNHZH
SR=SORT((SPL142)+(SPM*42)+(SPN**2))
XMDEC=ATAN2(9XM.SXL)*PI3
IF(XMDEC.LT.0.) XMDEC=XMDEC+390.
XALONG=ATAN2(SPM.SPL)4PI3
XALAT=ASIN(SPNISR)4PI3
XMINC =(ASIN(SXN/XR)) 4 P13
PRINT 90. TIME.XMDEC.XMINC
90 FORMAT(* MEAN DECLINATION AND INCLINATION FOR TIME * .I3. * ARE*
4. 2(1X.F9. 0))
PRINT 100. TIME. XALAT. XALONG
100 FORMAT (* MEAN SITE LOCATION FOR TIME i.I3.i IS *.2(1X.F9.1))
CL—CALCULAIEAMEAN_EOLES FROM-MEAN INC AND DEC - ~-n__.--.
C
C XP IS THE COLATITUDE.
XP'ATAN(2.1TAN(XMINC*PI2))
C XMLMBA IS MEAN LAT. XPHI IS MEAN LONG.
XMLM9A=ASIN((91N(XALAT*PI2)*COS(XP))+(COS(XALAT*PIZ)*SIN(XP)*
+COS(XMDEC*PIZ)))*PI3
XBETA=ASIN((SIN(XP)GSIN(XMDEC*PIZ))ICOS(XMLM9A*P12))iPIS
IF(COS(XP).GE.SIN(XALAT*PI2)*SIN(XMLM9A*PI2)) GO TO 110
XPNI = XALONG + 190. ~ XBETA

GO TO 120
110 XPHI = XALONG + XBETA

120 PRINT 130. TIME. XMUBA. XPHI
130 FORMAT( O MEAN PALEOPOLE FOR TIME * .12. 4 IS * .F9.1.F9.1)
150 IF (TIME .GE. 29) GO TO 140
GO TO 90
140 IF (NT.GT.0) PRINT 190.(NOTIME(J).J=1.NT)
190 FORMAT (11* NO DATA FOR TIMES *.29(1X.IZ))
STOP
END

Table A-V.

20

190

40

90

150

50

94

Data sort routine. Program used to print
a sorted data list.

PROGRAM JAYSORT (INPUT.OUTPUT.TAPEB)
INTEGER DATA (999.10). NOTII'E (29)
INTEGER TIME

RENIND9

I=0

1=1+1

READ (9.20) (DATA(I.J).J=1.10)

IF (EOF (9)) 5.30

FORMAT (A1.1X.12.1X.I4.1X.I4.1X.14.1X.14.4X.A10.A10.A10.A10)
99 TO 30

N=I~1

PRINT 190

FORMAT (1 HHAT PLATE?!)

READ 40.1PLATE

FORMAT(A1)

NT=0

TIME=0

TIME=TIME+1

DO 90 1‘11"

IF(TIME.GE.29) GO TO 50

IF (DATA(I.1).NE.IPLATE) GO TO 90
IF (DATA(I.2).NE. TIME) GO TO 90
FORMAT (A1.1X.IZ.1X.I4.1X.I4.1X.I4.1X.I4.4X.A10.A10.A10.A10)
CONTINUE

99 TO 90

CONTINUE

STOP

END

APPENDIX B

APPENDIX B

Glossary

Nizhn(yaya)(iye) - lower

Verkhyaya - upper

Melanocratonic - dark colored igneous rock rich in mafic
minerals (SO-60% mafic)

Olistostrome - Peyve (1973): what Soviet geologists call
olistostrome, European and American geologists call
melange

Externide - Smirnov (1971): miogeosynclinal area between
East European Platform in the west and the Main Uralian
Fault in the east. Includes Bashkir and Uraltau zone.

Internide - Smirnov (1971): eugeosynclinal, i.e., Western
Magnitgorsk and East Uralian Trough.

Tension - Khvorova et al. (1975): subsidence

Compression - Khvorova et a1. (1975): uplift

lst order - upwarps and downwarps

2nd order - anticlinoria and synclinoria

3rd order - anticlines and synclines

Phthanite - dull cryptocrystalline siliceous rock, i.e.,
silicified shale, schist and especially chert

Tributary — handedness measured facing downstream

95

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VITA
of

Jay Brian Silber

Personal Data

 

Date of Birth: March 5, 1956

Education

 

State University of New York, A & T at Delhi, 1974-1976,
A.A.S. (Mathematics)

State Uiversity of New York, University of Buffalo,
1976-1979, B.S. (Geology)

Michigan State University, 1979-1981, Geology

134

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