**DESCRIPTION OF MAP UNITS**

**NORTHEAST ASIA GEODYNAMICS MAP**

# TECTONOSTRATIGRAPHIC TERRANES

# (Arranged alphabetically by map symbol)

## 

## ACH Anui-Chuya terrane (Continental margin turbidite) (Early to Late Paleozoic) Gorny Altai (Altai)

The Anui-Chuya terrane consists of two adjacent blocks: northwestern
Anui block and southeastern Chuya block. The blocks are similar in the
structure of Cambrian-Silurian sections, but differ in composition and
age of Devonian rocks.

The oldest deposits are the Gornoaltaiskaya series that consists of
sand-shale flysch sequence with polymictic and oligomictic clastic
material. Also occurring are interbeds of siliceous-clay shale, which
increases to the west, farther from the North Asia Craton. A Middle and
Late Cambrian is indicated by sponge spicules in a marginal facies
adjacent to the Baratal terrane. Unconformably overlying is a Ordovician
and Silurian unit that consists of shelf carbonate and terrigenous
deposits that are similar to those in the coeval Charysh terrane. A
facies zonation, from shallow-water marine deposits to carbonate
platform deposits to deeper sedimentary deposits occurs. The age range
is from the Arenig, locally from the Middle and even Late Ordovician
through Late Wenlock to Pridoli.

Three generally unconformably overlying Devonian series occur. An Early
Devonian section consists of marine carbonate-terrigenous sedimentary
rocks with a facial zonation similar to that of the Late Ordovician and
Silurian section. Eifelian and Early Givetian tectonism is indicated by
disconformities at the base of the Eifelian, between the Eifelian and
Givetian, and between the early and late Givetian. The tectonism is
associated with Early Givetian volcanism with subaerial and submarine
eruption of calc-alkaline siliceous lava of the Kurota suite. Relative
stagnation occurred in the Late Givetian and Franian with accumulation
of fine-grainded terrigenous sand-clay-silt sedimentary rocks and
calcareous sedimentary rocks. The latter contain remnants of marine
fauna and fragments of continental flora in the lower horizons. Terrane
also contains Late Devonian and Early Carboniferous calc-alkaline,
plumasite, alkaline and subalkaline granitoids.

**REFERENCES**: Yolkin and others, 1994; Shokalsky and others, 1996;
Volkov, 1966; Buslov and others, 1998.

## AG Agardag terrane (Oceanic) (Vendian and Cambrian) (Southern Tuva)

Occurs in southern Tuva as a tectonic lens between the Tuva-Mongolian
superterrane and the Tannuols island-arc subterrane. Consists of three
units. The first unit consists of strongly-deformed, melange with
fragments of ophiolite including ultramafic rocks, gabbro, basalt,
plagiogranite, siliceous and siliceous-clay shale, and graywacke with a
U-Pb zircon isotopoic age of 570±1 Ma for the plagiogranite.
Volcanic-sedimentary varieties are considered as Kuskunug suite of,
probably, Vendian-Early Cambrian age. The second unit consists of
limestone with shale, sandstone and tuffaceous sandstone of the Karakhol
suite with sparse remnants of Early Cambrian archaeocyata and trilobites
in limestone and shale. The third unit mainly consists of conglomerate
(locally with boulders), gravelstone, and sandstone with the horizons of
olistostrome-like rocks of the Shurmak suite of possible Middle Cambrian
age. Vendian and Early Cambrian coarse-clastic rocks apparently mark the
beginning of collision in the associated island-arc system. Terrane is
interpreted as a back-arc basin deposited on oceanic crust that was
assoicated with a Vendian and Cambrian island arc system.

**REFERENCES**: Luchitsky, 1970, Berzin, 1979; Izokh and others, 1988;
Izokh, 1999.

## AI Amil terrane (Accretionary wedge, type A) (Vendian and Cambrian) (Western Sayan)

Consists chiefly of the Dzhebash series, that is more than 5,000 m
thick, that contains volcanic-sedimentary rocks that are metamorphosed
to greenschist facies. The lower part of the series is dominated by
paraschist derived from metamorphosed clay-, marl-, silt- and
sand-bearing sedimentary rocks with local rhythmic bedding. The upper
part is dominated by orthoschist derived from mafic and andesite tuff,
tuffaceous sandstone and volcanic flows, with local interbeds of marble,
mica-bearing piedmontite and magnetite quartzite. In the southern part
of the terrane, up section, the metamorphic schist is replaced by less
metamorphosed sandstone and phyllite. The volcanic-sedimentary unit is
interpreted as forming in the Vendian-Middle Cambrian as an accretionary
wedge in front of a volcanic island arc. The peak of high temperature
metamorphism is interpreted as occurring in the middle and late
Paleozoic from K-Ar isotopic ages 284 to 364 Ma for mica in the
metamorphic schist. Terrane is intruded by diorite-granodiorite of the
Bolsho Porog complex and granite-granosyenite of the Dzhoi complex. No
overlapping units occur. The Amil terrane, and companion Borus and
Dzhebash terranes, are interpreted as a system of large tectonic lenses
that are tectonically linked to the North-Sayan island-arc terrane.

**REFERENCES**: Zonenshain, 1963; Korobeinikov and Isakov, 1965;
Kazakov, 1967; Klyarovsky, 1972; Kheraskov, 1979; Berzin, 1995; Zaltsman
and others, 1996.

## AL Alambai terrane (Accretionary wedge, type B) (Vendian and Early Cambrian) (South Salair and northern Gorny Altai)

Consists of a sedimentary and volcanogenic assemblage of the Alambai and
Kivdin suites with bodies of strongly deformed and serpentinized dunite,
harzburgite, and lesser pyroxenite. Volcanogenic rocks consist of
chlorite and amphibole-bearing pillow-basalt, tuff and subvolcanic
bodies that are interpreted as within-plate basalt. Also occurring are
subordinate graywacke, siliceous shale, siliceous-clay shale, turbidite
and carbonate deposits. The blocks and lenses of carbonate rocks, with
subordinate volcanic rocks and siliceous-terrigenous rocks of the Kivdin
suite are interpreted as fragments of within-plate volcanic uplift
structures. A Vendian and Early Cambrian age is indicated by spores,
microphytoliths and algae remnants. To the east, the Alambai terrane is
thrust over early Paleozoic island-arc units in the Salair and Gorny
Altai regions. To the west, the terrane is overlapped by the Cenozoic
deposits of the West-Siberian plain.

**REFERENCES**: Grigor\'yev, 1988; Berzin and Kungurtsev, 1996;
Shokalsky and others, 1996; Tokarev and others, 1996; Nechaev and
others, 1999.

## AM Akiyoshi-Maizuru terrane (Accretionary wedge, type B) (Carboniferous and Permian) (Japan)

Consist chiefly of sandstone, conglomerate, and shale with chert,
basalt, limestone and ophiolite. Terrane is divided into two units the
Akiyoshi accretionary-wedge complex, and the Maizuru forearc formation.
The deposited Maizuru forearc formation is deposited on the Yakuno
Ophiolite. The Akiyoshi accretionary-wedge complex is mainly a chaotic
mixture of Middle to Late Permian trench-fill sedimentary rocks. Aso
occurring are Middle Permian pelagic chert, basalt, and limestone the
are the remants of Carboniferous to Permian seamounts. The chert, basalt
and limestone occur as allochthonous blocks in flysch and melange that
is interpreted as forming during the subduction of an oceanic plate.
Parts of the terrane is metamorphosed under high pressure conditions.
Overlying Triassic units are sandstone, shale, conglomerate, limestone,
and tuff of marine to non marine facies, locally with coal beds and
containing bivalves such as Halobia and Monotis, Triassic index fossils,
as the most dominant fauna. Jurassic shallow-marine to non-marine
sedimentary rocks overlie the Permian accretionary complexes and consist
predominantly sandstone, shale, conglomerate, and limestone, with
bivalve marine fauna.

**REFERENCES**: Hayasaka, 1990; Kanmera and others., 1990.

## AN Angurep terrane (Metamorphic) (Middle Silurian and older) (Southern Salair)

Consists of a series of nearly vertical tectonic sheets of the Alambai
accretionary-wedge complex. Composed of garnet amphibolite with
subordinate gneiss, marble, and quartzite. Three, fault-separated
sequences are recognized according to the degree of metamorphism: (1)
granulite and high-temperature eclogite; (2) high-pressure epidote
amphibolitE; (3) moderate-pressure epidote amphibolite. Unit also
exhibits retrograde greenschist metamorphism. Terrane is intruded by
zonal gabbro-pyroxenite bodies with a Sm-Nd isochron age of 421±1 Ma
age. Petrochemistry of igneous rocks indicates a high-sodium
low-alkaline series.

**REFERENCES**: Tokarev and others, 1996; Gibsher and others, 2000.

## ANV Aniva terrane (Accretionary wedge, type B) (Middle Triassic through early Late Cretaceous) (Southern Russian Far East)

Consists chiefly of a melange formed of: (1) lenses of Middle Triassic,
Jurassic, and Early Cretaceous oceanic high-titanium tholeiite, alkalic
basalt, and chert; (2) fragments of guyots with late Paleozoic and Late
Triassic limestone caps; (3) local exotic bodies of intensely
metamorphosed ultramafic and mafic rocks; and (4) a matrix of Albian to
Cenomanian turbidite and olistostromes. Individual cherty bodies range
from early Middle Triassic to early Cenomanian as determined by
radiolarian and conodont assemblages. Complexly folded and faulted and
metamorphosed to transitional blueschist-greenschist facies. K-Ar white
mica isotopic age of 54 Ma. Terrane contains a collision-related biotite
granite that intruded after metamorphism. Terrane is correlated in part
with Hidaka terrane of Hokkaido Island. The Aniva terrane is
tectonically paired to the East Sikhote-Alin volcanic-plutonic belt.

**REFERENCES**: Geology of the U.S.S.R., Sakhalin Island, 1970;
Dobretsov, 1978; Rikhter, 1986; Khanchuk and others, 1988; Bekhtold and
Semenov, 1990.

## AO Agoi terrane (Pre-Paleozoic) (Metamorphic) (Eastern Tuva)

Consists of biotite and biotite-amphibole schist and gneiss, often with
sillimanite, garnet and cordierite. Amphibolite, mica-bearing quarztite
and graphite-bearing marble occur locally. Metamorphosed to amphibolite
and epidote-amphibolite facies. Age of metamorphism and age of protlith
unknown. parental rocks has not been estimated yet. Terrane occurs
adjacent to Vendian-Cambrian island-arc units, within the large areas of
early Paleozoic granitic intrusions.

**REFERENCES**: Makhin, 1959; Parfenov, 1967; Il'in and Kudryavtsev,
1960.

## AR Argunsky terrane (Passive continental margin) (Paleoproterozoic through late Paleozoic) (Eastern Mongolia, Northeastern China, Transbaikalia)

## 

In Northeastern China, terrane consists mainly of two sets of
metamorphic rocks: (1) Paleoproterozoic and Mesoproterozoic metamorphic
rocks, chiefly biotite-hornblende-plagioclase gneiss, biotite
plagioclase gneiss, amphibolite, marble, quartz schist, and biotite
schist; that exhibit regional-grade, dynamo-thermal metamorphism of
lower amphibolite facies; and (2) Neoproterozoic metamorphic rocks,
chiefly sericite-chlorite-shale, sericite-quartz-shale, crystalline
limestone, ferrous quartzite, and diopside-plagioclase-gneiss, that
exhibit low-temperature regional dynamic metamorphism of lower
greenschist facies. Terrane is overlapped by Cambrian and Ordovician
marine sedimentary rocks, and by angular-unconformably overlying Late
Jurassic and Early Cretaceous siliceous-volcanic rocks. Bordered by
Derbugan fault to the southeast.

**REFERENCES**: Bureau of Geology and Mineral Resources of Inner
Mongolian Autonomous Region (Inner Mongolian GMRB), 1991; Dong Shenbao,
1993; Zhou Yuwei and others, 1993.

In eastern Mongolia and Transbaikalia region, terrane strikes northeast
from Eastern Mongolia and forms a unit that is 13,000 km long and from
200 to 250 km wide. Terrane borders on the Onon terrane (OS) to the
northwest, and the Nora-Sukhotin-Duobaoshan (ND), Mandalovoo-Onor (MD)
terrane to northeast, and east, and the Idermeg terrane (ID) to the
south and southeast. In some areas to the north, the tectonic borders of
the terrane are a left-lateral fault or overthrust, but in most cases
their tectonic nature of the contact is not clear.

The basement of the terrane consists of gneiss-like calc-alkaline
palingenic biotite granite and leucogranite of the Dyrbylkeiksky and
Urulunguebsky complexes. The U-Pb isotopic age of the former is 740±20
Ma (Bibikova and others, 1979), the Rb-Sr isotopoic age is 782±6 Ma
(Rutshtein and Chaban, 1997). The Rb-Sr isotopoic age of the latter is
850±20 Ma (Bibikova and others, 1979). These weathered granitoids are
overlain by middle Riphean sedimentary rocks of the Daurian series that
consists of metamorphosed sandstone, siltstone, marble, and dolomite,
limestone, siliceous rocks, and carbonaceous shale. The top of the
sedimentary section consists of the Byrkinsky suite that contains
layered bodies of basalt, rhyolite, and picrite metamorphosed to
greenschist facies (Rutshtein and Chaban, 1997). The basalt is either a
low-Ti variety similar to N-MORB, and a high-Ti variety similar to
T-MORB (Gusev, Peskov, 1996). The volcanic rocks are interpreted as
forming during rifting of a passive margin. The basement of northeast
part of terrane consists mainly of two sets of metamorphic rocks: (1)
Paleoproterozoic metamorphic rock consisting of lower amphibolite
facies, biotite-hornblende-plagioclase gneiss, biotite-plagioclase
gneiss, amphibolite, marble, quartz schist and biotite schist; (2) the
Neoproterozoic metamorphic rock consisting of lower greenschist facies
sericite-chlorite-schist, sericite-quartz-schist, marble, ferrous
quartzite, and diopside-plagioclase-gneiss (Dong Shenbao, 1986).

Overlying Vendian and Cambrian sedimentary rocks consist of the
Gazimiursky sedimentary basin that forms part of the Argunj series. The
lower part of the section consists of coarse-grained quartz sandstone
and gravelstone that are succeeded by intercalated dolomite, limestone,
marl, and terrigenous rocks. The age of is derived from abundant fauna,
including archaeocyates, trilobites, brachiopods, bivalves, and
micro-gastropods (Anashkina and others, 1997). Overlying Silurian
through Early Carboniferous rocks consists of terrigenous sedimentary
rocks with minor carbonate of the Gornozerentuy sequence, and the
Talovsky suite that contains terrigenous sedimentary rocks with rare
interbeds of greenstone and interbeds of intermediate and siliceous
tuff. Also occurring is the Alenuysky complex containing Carboniferous
intermediate and siliceous subvolcanic bodies. Also occurring are rare
small layered massifs of gabbros and monzonites of the Late
Carboniferous Taininsky complex that is interpreted as forming during
intraplate activity. The youngest rocks in the terrane are late
Paleozoic sedimentary rocks of the Early-Borzja fore-arc basin (Early
Carboniferous through Early Triassic), granitoids of the Permian
Undinsky complex of the North-Gobian volcanic-plutonic belt, and
sedimentary rocks of marine molasse of the Early Jurassic Upper Borzja
sedimentary basin.

The overlapping and stitching complexes are continental molasse of the
Middle Jurassic Upper Gazimur suite, and sedimentary and
volcanic-plutonic rocks of Trans-Baikalian-Daxinganling
sedimentary-volcanic plutonic belt of Middle Jurassic through Early
Cretaceous age. The age of accretion of the terrane to the eastern North
Asia Craton is defined from the time of formation of continental molasse
of the Middle Jurassic Upper Gazimur suite.

**REFERENCES**: Kotlyar and Popeko, 1974; Kozlov, 1972; Rutshtein and
Chaban, 1997; Bibikova and others, 1979; Dong Shenbao, 1986; Efremov and
others, 1998; Gusev and Peskov, 1996; Zorin and others, 1998a.

## AT Altai terrane (Continental margin turbidite) (Precambrian and Cambrian through Devonian) (Southern Gorny Altai, Northwest China, Mongolia)

In northwest China forms the main part of Altay Mountains, and consists
of two parts: (1) Precambrian migmatite, schist, marble, and other
metamorphic rocks with algae and micro-flora fossils; (2) Ordovician,
Silurian, and Devonian flysch, that unconformably overlaps the
Precambrian basement, and consists mainly of metasandstone,
metasiltstone, metashale, metatuff, metamorphosed clastic rocks, chert,
and other sedimentary rocks, with local brachiopoda, anthozoan corals.
Carboniferous marine and limnic terrigenous rocks unconformably overlap
the Altay terrane. The southern part of Altay terrane is interpreted as
a late Paleozoic continental margin arc.

**REFERENCES:** Yang Sennan, 1984; Ren Jishun and others, 1980; Bureau
of Geology and Mineral Resources of Xinjiang Uygur Region (Xinjiang
GMRB), 1990.

In western Mongolia, consists chiefly of: (1) Middle to Late Cambrian
sandstone, siltstone and shale grading upward into coarse-grained
deposits that are more than 6,000 m thick (Altay series); (2)
unconformably overlying Silurian conglomerate, sandstone, siltstone,
tuff with minor basalt, andesite, rhyolite, and limestone containing
brachiopods and tabulata corals. Middle to Late Cambrian rocks are
metamorphosed to greenschist facies and strongly deformed into northwest
trending, open to isoclinal folds. Preaccretion granitic rocks consist
of calc-alkalic diorite, granodiorite, and granite of Tsagangol complex,
that yield K-Ar ages of 400 to 456Ma. The Altay terrane is overlain by a
Devonian sedimentary-volcanic-plutonic assemblage, Early Carboniferous
shallow marine sedimentary rocks, Permian volcanic-sedimentary rocks,
and Early to Middle Jurassic coarse nonmarine sedimentary deposits.
Postaccretion granite rocks include Late Devonian, Middle to Late
Carboniferous and Early Permian granite, leucogranite, and alaskite.In
Mongolia, the Altai terrane is interpreted as a continental margin
fragment that was tectonically linked to the Hovd continental-margin
turbidite terrane in the Devonian.

**REFERENCES**: Berzin., 1995; Volochkovich and Leont'ev, 1990; Byamba
and Dejidmaa, 1999; Demin and Demin., 1993; Dergunov and others, 1980,
1989; Dobretsov and others, 1995; He Gouqi and others, 1991, Gavrilova
and others., 1975, Windley and others, 1994, Zonenshain and others,
1990.

In the southern Gorny Altai, consists of Middle-Late Cambrian thick
sand-shale flysch that formed at the foot of a continental slope. The
lower part of the section consists of gray and green-gray,
quartz-plagioclase clastic material. Upwards, the rocks are more
polymictic. The flysch-like unit may be underlain by ophiolite and
locally by island-arc rocks. Middle and Late Ordovician deposits with
marine fauna fossils opccur adjacent to the southwestern margin of the
terrane, range up to 2000 m thick and consist of gray and green and rare
red, polymictic calcareous sandstone, shale, and calcareous siltstone,
with gravelstone and conglomerate interbeds and limestone lenses. The
relationship to the Cambrian deposits is unclear. Silurian and Devonian
deposits occur in several parts of the terrane and consist of sandstone
and siltstone, and molasse with limestone lenses of Early-Late Silurian
age as indicated by coral, brachiopods, trilobites, and conodonts. The
Silurian deposits disconformably overlap the Cambrian flysch that is
metamorphosed to greenschist facies in the pre-Silurian. The molasse
deposits are coarse-clastic rocks (conglomerate, gravelstone,
coarse-grained sandstone), mainly siliceous-quartz composition, and
subordinate siltstone, shale, marl, and limestone that contain Wenlock
and Ludlow brachiopods, rugose corals, and Tabulata corals. In the
southwestern part, the Silurian deposits are conformly overlapped by
Lokhkov limestone (Sarymsaktin suite). The central and eastern areas are
partly covered by Early-Middle Devonian volcanic-sedimentary rocks.

Locally, the Cambrian sequences are zonally metamorphosed to amphibole
facies that occurred during middle Paleozoic strike-slip faulting and
related tectonic piling. An east-west-striking metamorphic zone in
southern Gorny Altai, in the South-Chuya ridge area, contains the
youngest metamorphic event, with a Rb-Sr isotopic age of 357±21 Ma for
tourmaline-bearing granite. In the northwest, the intrusive units are
dominated by possibly two or more generations of Devonian plumasite
low-alkaline granite with U-Pb isotopic ages of 401±4 and 375±29 Ma, and
Jurassic raremetal-plumasite granite with Rb-Sr isotopic age of 204±2,
and U-Pb isotopic ages of 182±19, and 196±4 Ma.

**REFERENCES**: Berzin and Dobretsov, 1994; Bespajev, 1997; Dergunov and
others, 1980; Grigor\'yev, 1988; Kozlov, Dubatolov, 1994; Plotnikov and
others, 1998; Shokalsky and others, 1996; Vladimirov and others, 1997;
Volochkovich and Leontjev, 1964; Zonenshain and others, 1990.

## AV Atamanov terrane (Granulite-paragneiss) (Paleoproterozoic) (Yenisey Ridge)

Occurs in the southern part of the South Yenisey Ridge to the east of
the Kuzeev terrane. Extends for 70 km and ranges up to 25 km wide. To
the east, the terrane is intruded by Taraka granite with a isotopic age
of 1780±10 Ma (Bibikova and others, 1993). Consists mainly of
high-aluminous garnet-biotite, cordierite-garnet-biotite,
garnet-sillimanite-cordierite gneiss and granulite (Nozhkin, 1999).
Migmatite, gneiss, and pegmatite are widespread. Protoliths are clay and
polymictic sedimentary rocks (Precambrian..., 1986; Popov, in press).
The relationships with Taraka granite and granulite metamorphism
suggests the terrane is Paleoproterozoic.

**REFERENCES**: Precambrian \_\_\_, 1986; Nozhkin, 1999; Popov, in
press.

## AY Ayansk terrane (Passive continental margin) (Ordovician through Late Carboniferous) (Yakutia)

Consists chiefly of Ordovician, Silurian, Devonian, and Late
Carboniferous shallow-marine limestone, quartz sandstone, siltstone,
diabase, conglomerate, breccia, dolomite, and argillite (Aldomsk,
Lantarsk, Ulukansk, Tanchinsk, and Jikandisnsk suites). Also locally
contains Early and Late Devonian, deep-marine tuffaceous rocks, and
radiolarian chert, but relation to shallow-marine rocks is unclear.
Paleozoic rocks are intruded by inferred late Paleozoic gabbro. The Late
Ordovician, Silurian, and Middle and Late Devonian limestone contains
abundant brachiopods. Late Carboniferous argillite contains Angara
flora. Late Devonian diabase, conglomerate, and breccia may be
rift-related. Paleozoic stratigraphic units are unconformably overlain
by Late Jurassic andesite and volcaniclastic rocks of Uda
volcanic-plutonic belt (unit ud) which links Ayansk terrane to Siberian
platform.

**REFERENCES**: Krasny and others, 1966; Shilo, 1982; Zmievsky, 1990.

## BA Beitianshan-Atasbogd terrane (Island arc) (Devonian through Carboniferous) (Northwest China, Mongolia)

## 

In northwest China, consists of: (1) intermediate-mafic,
intermediate-siliceous, siliceous volcanic rocks, chert, limestone,
tuff, sandstone, and siltstone, with Devonian brachiopods, anthozoan
marine corals; (2) andesite-porphyry, intermediate-siliceous tuff,
tuffaceous sandstone, siltstone, basalt, and interbedded flysch and
limestone with Carboniferous fusulinids and brachiopods. Unconformably
overlapping units are Permian andesite, rhyolite, sandstone, limestone,
and conglomerate. The Early Permian strata contain brachiopods and the
late Permian strata contain flora.

**REFERENCES:** Ren Jishun and others, 1980; Bureau of Geology and
Mineral Resources of Xinjiang Uygur Aut. Reg.(Xinjiang GMRB) (1990).

In southwestern Mongolia, consists of: (1) undated biotite gneiss,
migmatite, orthogneiss, amphibolite, metagabbro, metadiorite,
metarhyolite, and metagranite; (2) Ordovician and Silurian greenschist
facies metamorphosed sandstone, siltstone, argillite, phyllite, chert,
and quartzite, and minor marble and pillow basalt (Tomort Formation);
(3) Early and Middle Devonian conglomerate, sandstone, siltstone,
basalt, andesite, dacite, rhyolite, tuff, breccia, and radiolarian
chert, and rare fossiliferous limestone lenses (Ehiyn gol Formation);
(4) Mississippian conglomerate, sandstone, siltstone, limestone lenses
with brachiopods and bryozoan. The terrane is intruded by Silurian(?)
tonalite, granodiorite, monzodiorite, and granite (Naransevestey
Complex) and Late Devonian and Early Carboniferous granodiorite,
quartz-diorite, and granite, minor gabbro and diorite (Gobi-Tienshan
Complex).

Overlap and stitch complexes are Pennsylvanian and Early Permian
volcanic and volcaniclastic rocks, and the Noyon foreland basin that
contains Late Permian to Jurassic alluvial and lake sedimentary rocks,
and alkaline granite plutons (Transaltai Complex). Terrane was formerly
interpreted as western part of South Gobi microcontinent (Zonenshain,
1972; Ruzhentsev, 1985) or a northern slope and rise (Ruzhentsev and
others, 1987). This study interprets the terrane as an intensely
deformed and metamorphosed, displaced fragment of an island arc and
forearc or backarc basin.

**REFERENCES:** Zonenshain, 1972; Ruzhentsev, 1985, Ruzhentsev and
others, 1987; Badarch, 1990.

## BD Badzhal terrane (Accretionary wedge, type B) (Permian through Jurassic) (Southern Russian Far East)

## 

Southern part of the terrane consists of : (1) Paleozoic limestone
olistoliths embedded in a clastic matrix; (2) chert inclusions with
Permian and Triassic conodonts and Mesozoic radiolarians; (3) turbidite
deposits with Late Triassic *Monotis* and *Holobia*, and Middle and Late
Jurassic pelecypods and ammonites; (4) chert and siliceous shale with
Late Triassic and Jurassic radiolaria and conodonts; and (5) small
lenses of mafic volcanic rocks. Previously studies indicated terrane
consisted of widespread Carboniferous and Permian clastic rocks and
limestone with macro- and microfauna, chert, mafic volcanic rocks, and
Triassic and Jurassic clastic and rare volcanic units. Mesozoic units
occur mainly in the eastern and southeastern part of the terrane.

Terrane is interpreted as a Triassic to Middle Jurassic accretionary
wedge complex that consists of tectonically intermixed oceanic and
continental slope deposits. Limestone units, that contain Carboniferous
and Permian Tethyan fauna, are interpreted as caps to seamounts.
Mesozoic deposits in the southeastern part of the terrane may constitute
a subterrane. A series of metamorphic domes with amphibolite-facies
metamorphism occur near the boundary with the Turan terrane of the
Bureya superterrane. The domes are interpreted as forming during
formation of the accretionary complex.

Postaccretion rift-related Cenozoic alkalic basalt and sedimentary rocks
of the Sakhalin-Primorye volcanic belt occur in narrow, north-striking
basins within the terrane. The Badzhal terrane is interpreted as
tectonically linked to the Khingan-Okhotsk active continental margin to
the south. The Cretaceous granitic and volcanic rocks of the
Khingan-Okhotsk belt link together the Turan and Malokhingansk terranes
of the Bureya superterrane, and the Badzhal, Galam and Ulban terranes.

**REFERENCES**: Krasny, 1966; Romanchuk and Maiboroda, 1974; Shevelev
and Kuzmin, 1990; Natal'in, 1991, 1993; Zablotsky and others, 1991.

## BG Bayanleg terrane (Accretionary wedge, type A) (Ordovician to Devonian) (Gobi Altay)

## 

Consists chiefly of an intensely-deformed, thick assemblages of
Ordovician to Devonian sandstone, siltstone, shale, chert, tuff, and
rare coral and crinoid-bearing limestone that contain small bodies of
ultramafic rocks and gabbro (Bayanleg ultramafic belt). Intensely
faulted, sheared, mylonitized, and metamorphosed to greenschist and
amphibolite facies, and intruded by sills of gabbro, diorite and
foliated biotite granite. K-Ar isotopic ages are 430 to 450 Ma for the
amphibolite, 395 to 330 Ma for gabbro (Pinus and others, 1981, 1982).
Terrane is interpreted as a subduction zone assemblage that was
tectonically linked to the Mandalovoo island arc terrane.

**REFERENCES:** Pinus and others, 1981, 1982; Kuznetsov, 1983;
Ruzhentsev and others, 1987; Badarch, 1990.

## BH Bayanhongor terrane (Oceanic) (Neoproterozoic) (Western Mongolia)

## 

Forms a northwest-trending, discontinuous, narrow belt that consists of
a large ophiolite allochton that structurally interleaved with the
southern part of the Orhon terrane. Consists of two synformal belts
bordered by serpentinite melange zones. The largest and northern synform
consists of serpentinite melange with a length of up to 300 km and a
width of 1-10 km. The second southern synform includes small zones of
serpentinite melange that vary from 5 to 10 km long, and range up to 5
km wide. The ophiolite complex includes metaperidotite, cumulate,
gabbro, sheeted dikes, and basalt pillow. Sm-Nd whole rock isotopic age
from gabbro is 569 Ma (Kepezhinskas and others, 1991).

The metaperidotites consist of harzburgite serpentinite, and the
cumululate rocks consist of alternating harzburgite, dunite, werlite,
clinopyroxenite, and less common orthopyroxenite. Thickness of layers
varies from 1.5 to 40 m, with a total thickness of 350 m. In the
cumulate rocks are small lenticular bodies of rodingite gabbro (lower
gabbro) at the base, and individual small dikes of rodingite diabase at
the top of the section. The upper gabbro consists of a 50 m layer of
mainly mesocratic gabbro both massive and with local pegmatoid
structure. Sheeted dikes consist of aphyric and porphyritic basalt and
diabase with screens of gabbro. Thickness of sheeted dikes varies from
500 m to 1200 m. Pillow lava unit consists of plagiophyric and aphyric
basalt and diorite. Terrane is moderately to intensely folded and
thrust-faulted, and structurally overlies highly-deformed sedimentary
rocks of Orhon terrane. Terrane is overlain by Late Ordovician,
Silurian, Devonian, Early Carboniferous sedimentary rocks, and is
intruded by early and late Paleozoic granitic rocks. The fault
juxtaposition of the Early Carboniferous sedimentary rocks requires
extensive post Carboniferous tectonic displacement within the terrane.
Terrane is interpreted as a fragment of oceanic crust that was
tectonically linked with Orhon and Zag Haraa terranes in early
Paleozoic.

**REFERENCES**: Perfiliev and Kheraskov, 1980; Kopteva and others; 1984;
Kepezhinskas and others; 1991; Ryazantsev, 1994; Kotov and others, 1995;
Teraoka and others, 1996;Dergunov and others; 1997; Takahashi and
others, 1998; 1999; Takahashi and others, 1999.

## BI Birusa terrane (Paragneiss) (Paleoproterozoic to Neoproterozoic) (Eastern Sayan)

Extends in a northwestern direction for 350 km long and varies from 70
to 100 km wide. Consists of the Khailamin and Alkhadir units:. Khailamin
unit consists of biotite, garnet-biotite gneiss, plagiogneiss,
amphibolite, two-pyroxene, and pyroxene-hornblende gneiss. Migmatites
are widely distributed, and amphibolite derived from mafic metavolcanic
rocks and charnockite occur locally. Metamorphic grade ranges from
amphibolite to granulite facies. The lower part of the Alkhadir unit
consists of high-magnesia orthoamphibolite, similar to metakomatiite,
serpentine-chlorite and biotite-actinolite schist, and overlying marble
and high-alumina mainly biotite-garnet gneiss.

A well-marked metamorphic, structural and stratigraphic unconformity
occurs between these units. Most researchers interpret that the age of
Khailamin unit as Archean and Paleoproterozoic(?), and the age of the
Alkhadir unit as Paleoproterozoic, Mesoproterozoic, and
Neoproterozoic(?). Terrane is unconformably overlapped by Neoproterozoic
terrigenous-carbonate deposits (Karagas and Oselok units) and in the
northeast by the Paleoproterozoic and Mesoproterozoic
terrigenous-carbonate deposits, including Devonian volcanogenic and
volcanic-sedimentary rocks. The terrane is intruded by biotite, two-mica
and muscovite granite, and leucogranite of the Sayan complex, and by
Early Devonian biotite, subalkaline and alkaline granite and
granosyenite. It is assumed that the age of Sayan granite is the
Paleoproterozoic.

**REFERENCES**:.Galimova and Bormotkina, 1983; Sez'ko, 1988; Brintsev,
1994; Nozhkin, 1999.

## BK Belaya-Kitoy terrane (Metamorphic) (Archean?) (Eastern Sayan)

## 

Consists of several northwest-trending tectonic lenses and sheets that
dip steeply (70-85°) to the southwest. Chiefly composed of gneiss with
variable amounts of mica, amphibole, clino-orthopyroxene, and garnet,
and less abundant amphibolite, marble, and calciphyre with gneissic
granite and alaskite. Blastomylonization and metamorphic diaphthoresis
of epidote-amphibolite and greenschist facies occur locally. Metamorphic
rocks are similar to Archean units of adjacent areas in the North Asian
Craton, from which the Belaya-Kitoy terrane is separated by the large,
regional, strike-slip Main Fault in the Eastern Sayan. K-Ar isotopic
ages of biotite and amphibole range from 206 to 478 Ma, with a peak of
285-312 Ma. The ages are interpreted as reflecting a superposed thermal
event in a late Paleozoic strike-slip zone.

**REFERENCES**: Polkanov and Obruchev, 1964.

## BL Baladek terrane (Metamorphic) (Paleoproterozoic through Ordovician) (Southern Russian Far East)

Consists chiefly of a crystalline basement complex and younger
stratified units. Basement complex consists of anorthosite,
gabbro-anorthosite, gabbro, gabbro-norite and pyroxenite (Malotokhikansk
and Tokhikansk complexes). Anorthosite is intruded by granite and
granodiorite with preliminary U-Pb isotopic ages ranging between 2.2 and
2.6 Ga, and K-Ar isotopic ages ranging between 964 and 365 Ma.
Unconformably overlying stratified units are: (1) Early Cambrian red
conglomerate, sandstone, siltstone, basalt, and limestone (Shevlinsk and
Usttimptonsk suites); (2) Late Cambrian limestone, sandstone and
siltstone; (3) thick units of sandstone, siltstone, conglomerate,
limestone, and marl that contain Early Ordovician algae and yield K-Ar
glauconite ages of 491 and 495 Ma.; (4) Mississippian sandstone; and (5)
Triassic and Early to Middle Jurassic marine clastic rocks that
unconformably overlie older rocks and are interpreted as a forearc basin
to the Uda volcanic-plutonic belt, part of the Mongol-Okhotsk active
continental margin, that occurs along the Stanovoy block of the North
Asian Craton. The terrane is unconformably overlapped by Late Jurassic
marine clastic deposits and Early Cretaceous nonmarine clastic deposits
(Uda-Zeya sedimentary basin) that links the Baladek terrane with the
North Asian Craton Margin. Early Cambrian archaeocyatheans of terrane
are similar to those of Siberian Platform and differ from
archaeocyatheans in limestone olistoliths in the nearby Galam terrane.
The Baladek terrane bounded to south by the Uligdansk dextral-slip fault
and is interpreted as a fragment of the North Asian Craton Margin.

**REFERENCES**: Kirillova and Turbin, 1979; Karsakov and others, 1987;
Belyayeva, 1988; Martynyuk and others, 1990; Krasnyi and others, 1996.

## BLK Belokurikha terrane (Metamorphic) (Late Permian and older) (Northern Gorny Altai)

Forms a tectonic sheet that is thrust over the accretionary wedge
Alambai terrane. Chiefly composed of metapelite, lesser amphibolite, and
quartz-banded iron ores metamorphosed to epidote-amphibolite facies. Age
of parental rocks and initial stage of metamorphism not yet estimated.
Locally, these rocks experienced superimposed low-pressure
high-temperature metamorphism and granitization as indicated by U-Pb
zircon isotopic ages of 311±Ma. Terrane is intruded by a massif of Late
Permian and Triassic high-potassium granite with a U-Pb zircon isotopic
age of 232±4.7 Ma, or a Rb-Sr whole rock isotopic age of 245±8 Ma. To
the the north, the terrane is overlapped by Cenozoic sedimentary rocks.

**REFERENCES**: Blyuman and Petrov, 1973; Kargopolov and others, 1995;
Shokalsky and others, 1997; Vladimirov and others, 1997.

## BM Baikal-Muya terrane (Island arc) (Neoproterozoic) (Transbaikalia)

## 

Extends from Lake Baikal in the west)to Vitim River and consists of
ophiolite fragments that occur in tectonic slabs and wedges. Ophiolite
consists of basalt, hemipelagic sedimentary rocks, gabbro and alpine
type ultramafic rocks. Basalts are N-MORB, E-MORB, and IAB types. Age of
ophiolite unknown, but ophiolite is intruded by Neoproterozoic island
arc magmatic rocks. The island arc complex consists of
basalt-andesite-plagiorhyolite (upper Kilyansky suite),
gabbro-plagiogranite intrusive bodies, tuffaceous-volcaniclastic
turbidites marginal to the arc rocks. The ophiolite and island arc
complexes are metamorphosed to greenschist facies. Ophiolite and island
arc complexes are locally deformed into steep isoclinal and inverted
folds with variably-oriented axes. The island arc complex contains
Riphean microfossils (Stanevich, Perelyaev, 1997) and exhibits U-Pb
zircon isotopic ages of 923 Ma for plagiorhyolite (Konnikov and others,
1994), Sm-Nd isotopic age of 825 Ma for gabbro (Isokh and others, 1998),
Rb-Sr isotopic ages of 774 and 773 Ma for gabbro (Tsygankov and others),
and Rb-Sr isotopic ages of 880 and 730 Ma for plagiogranite. Accretion
of the terrane to the North-Asian Craton is interpreted as occurring at
the end of Riphean. Accretion was associated with formation of
intermontane depressions filled with continental sub-alkaline basalt and
rhyodacite, tuff, and coarse clastic sedimentary rocks (Padrinsky
series, Tuluinsky suite, Zhanokinsky complex). The Padrinsky series is
deformed into linear folds with shallow-dipping (30°) limbs. The
Zhanokinsky volcanic complex dips horizontally and subhorizontally.
Close to fault zones, the folds are steep, vertical and inverted.
Comagmatic with extrusive rocks are gabbro, diabase, and leucogranite
(Vitim complex). The Rb-Sr isotopic age of the extrusive rocks is
765-712 Ma (Bulgatov, 1983; Zagruzina and others, 1984). Overlying and
intruding the terrane are Vendian-Cambrian non-metamorphosed
terrigenous-carbonate sedimentary rocks in the Upper Angara sedimentary
basin and granite of the Konkudero-Mamakan complex with U-Pb zircon
isotopic ages of 556 and 470 Ma (Sryvtsev and others, 1992) for
alkaline-syenite (Synnyrsky complex), lamprophyre (Kadali-Butuinsky
complex). Seismic data indicate that fragments of terrane are underlain
at depth by oceanic crust.

**REFERENCES**: Bolonev and others, 1983; Bulgatov, 1983; Bulgatov,
1988; Izokh and others, 1988; Sryvtsev and others, 1992; Konnikov and
others, 1994; Zagruzina and others, 1984; Bulgatov, 1995; Stanevich and
others, 1997; Bulgatov and Zaitsev, 1998; Tsygankov and others, 1998.

## BR Baratal terrane (Accretionary wedge, Type B) (Late Neoproterozoic through Early Cambrian) (Southeastern Gorny Altai)

## 

Consists of a combination of tectonic sheets and nappes that dip to the
southwest and are thrust over Vendian-Early Cambrian island-arc units to
the southeast. From lower to upper, the imbricated-thrust structure
consists of several units. (1) An ophiolitic melange that consists of
harzburgite, serpentinite, garnet amphibolite, eclogite, basalt and
greenschist with barroisite, stilpnomelane, and glaucophane. K-Ar
isotopic ages of amphiboles are 535±24 Ma for eclogite are 487±22,
473±13 Ma for garnet amphibolite, and 523±23 Ma for garnet-free
amphibolite. K-Ar isotopic ages for chlorite and chlorite-muscovite
matrix from the greenschist are 540±24 and 567±11 Ma, respectively. The
garnet amphibolite and eclogite are N-MORB type. (2) A late
Riphean-Early Cambrian(?) sedimentary-volcanogenic assemblage that
contains a series of sheets of marine and oceanic island basalt (main
part of the Arydzhan and Sagalak suites), limestone, shale, chert,
sandstone, and polymictic and carbonate olistostromes, and a local
siliceous-carbonate assemblage. And (3) alternating tectonic sheets of
chert, marine slide breccias of siliceous composition (olistostromes),
shale, and basalt.

An imbricated nappe consists of Vendian-Early Cambrian
siliceous-carbonate rocks (Baratal suite) with lenses of polymictic
olistostromes in the base. The total thickness of the imbricated-thrust
structure is greater than 10 km. In the southwest, the terrane is
overlain by the Middle and Late Cambrian continental margin molasse with
olistostrome horizons, and locally by Early and Middle Devonian
sedimentary-volcanogenic rocks that were part of an active continental
margin. The terrane is cut by northwest-striking strike-slip faults of
late Paleozoic-early Mesozoic? age.

**REFERENCES**: Gusev, 1991; Dobretsov and others, 1992; Buslov and
others, 1993; Buslov and Watanabe, 1996.

## BRG Barguzin terrane (Metamorphic) (Late Neoproterozoic) (Transbaikalia)

## 

Stratified units are as follows. (1) The Ulokitsky suite that consists
of tuffaceous-basalt-terrigenous rocks, flood basalt, and gabbro-diabase
sills. (2) The overlying Nyandoninsky sandstone-shale suite of
interbedded sandstone, limestone, flood basalt, tuff, gabbro-diabase and
gabbro-diabase. The igneous rocks have high Ti and P contents, are
enriched in light REE, and are close in composition to continental rift
basalt. And (3) the Barguzin shale sequence suite. Total thickness is
7,000 m. The Nyandoninsky and Barguzin suites contain microfossils of
the Middle and early Late Riphean age (Dolnik and others, 1990), and are
metamorphosed from greenschist to amphibolite facies around the contact
zone of the Barguzin-Vitim batholith that contains a staurolite zone
from 5-15 km width (Bolonev and others, 1983). Farther from from the
contact, this zone is replaced by a garnet zone
(staurolitechlorite-muscovite and garnet subfacies) with a width of
10-15 km. At a greater distance from the contact of batholith is a
chlorite-actinolite-biotite zone with a width of 10-20 km. The last
subfacies is characteristic of the rocks of all suites, even for: rocks
of the lowest Ukolkitsky suite. The zonal metamorphism is a
kyanite-sillimanite facies series. The sedimentary rocks in the terrane
are deformed into northeast-trending linear fold. The terrane is
overlapped by Vendian-Cambrian non-metamorphosed, variegated
basalt-terrigenous, terrigenous, and fauna-bearing carbonate sedimentary
rocks of the Upper Angara sedimentary basin (Bolonev and others, 1983).
Early, middle and late Paleozoic granite batholiths intrude the terrane
and have U-Pb zircon isotopic ages of 440, 425, 390, 307, 301-300 Ma
(Rytsk and others, 1998). Seismic data indicate a continental crustal
basement below the terrane (Bulgatov, 1988).

**REFERENCES**: Bolonev and others, 1983; 1983; Bulgatov, 1998; Dolnik
and others, 1990; Rytsk and others, 1998.

## BS Borus terrane (Accretionary wedge, type B) (Early Cambrian) (Northwest Sayan)

## 

Consists of the following sequences. (1) An ophiolitic assemblage with a
lower part of serpentinized dunite, harzburgite, lherzolite, and lesser
werlite with small lenses of gabbro-amphibolite, and an upper part of
metabasalt, tuff, siliceous and black shale, phyllite and clastic rocks
that formed from erosion of volcanic-siliceous deposits (Chingin suite).
Blocks of high-pressure rocks, jadeite and garnet amphibolite, occur
within the serpentinite melange. (2) A presumed island-arc assemblage of
weakly metamorphosed pyroxene porphyry, mafic tuff, volcaniclastic
rocks, siliceous shale, and marble-like limestone with sparse Early
Cambrian archeocyata. The Kantegir gabbro-diorite-plagiogranite
assemblage, that occurs in the ultramafic rocks, is interpreted as part
of an island-arc. Kantegir assemblage is correlated with the Main massif
granitoids of the North-Sayan terrane. And (3) coarse-clastic deposits,
ranging in size from boulder conglomerate to sandstone, and tuffaceous
rocks of unknown age, with clasts of mafic volcanic rocks, chert,
limestone and ultramafic rocks. These coarse-clastic deposits occur in
small, fault-bounded zones and less deformed and metamorphosed compared
to the other units. The Borus terrane is intruded by Middle Silurian and
Early Devonian granitoids of the Bolshoy Porog and Dzhoi complexes.

**REFERENCES:** Isakov and Korobeinikov, 1969; Sobolev and Dobretsov,
1977; Kheraskov, 1979.

## BU Bureya terrane (Metamorphic) (Neoproterozoic through Triassic) (Southern Russian Far East)

## 

Occurs in the northwestern part of the Amursk superterrane. Consists
mainly of early Paleozoic metamorphic core complexes composed of large
lower and the upper units. The lower unit (Amursk and Gudzhalsk suites)
consists of gneiss, schist, marble, quartzite, and amphibolite that are
metamorphosed to amphibolite facies. The upper unit consists of marble,
quartzite, and metasandstone that is metamorphosed to greenschist
facies. In the northwestern and southeastern parts of the terrane, near
the boundary with the Nora-Sukhotinsk and Malokhingansk terranes,
metamorphosed gabbro, pyroxenite, and peridotite intrude gneiss and
schist, amphibolite, and marble. Older, weakly metamorphosed overlap
assemblages are (1) silicic and intermediate volcanic rocks, sandstone,
and siltstone (Turansk suite); (2) Neoproterozoic limestone (Melgiysk
suite) with plant microfossils; (3) Cambrian clastic rocks and limestone
(Allingsk and Chergelensk suites) with Archaeocyatheans. Younger overlap
assemblages are Middle and Late Devonian clastic rocks with marine
faunas that form wall rocks to abundant late Paleozoic and possibly
early Mesozoic granitic rocks. Widespread early Paleozoic granitic rocks
(Kiviliysk and Sularinsk complexes) intrude the terrane and consist of
(1) predominantly biotite and hornblend-biotite granite, granodiorite,
and diorite of the subduction-related Tyrma-Bureinsk complex; (2) minor
Permian granosyenite, syenite, quartz syenite, and coeval volcanic
rocks; and (3) large plutons of leucogranite and silicic volcanic rocks
of possibly Triassic age. The large Bureya sedimentary basin overlaps
the eastern part of the terrane. The narrow Umelkan-Ogodzhin belt
overlies the northern flank of the terrane and sutures the Turan, Mamyn,
Gonzha, and Oldoi terranes. The Cretaceous Khingan-Okhotsk
volcanic-plutonic belt intrudes the southern part of the terrane.

**REFERENCES**: Sigov, 1973, Zmiyevsky, 1979, Kozlovsky, 1988, 1980,
Natal'in, 1991.

## BY Baydrag terrane (Cratonal) (Neoproterozoic and older) (Northwest Mongolia)

## 

Consists chiefly of Early Precambrian crystalline basement and Riphean
sedimentary cover. The Precambrian basement comprises of the Baydrag and
Bumbuger structural-metamorphic complexes. The Byadrag complex consists
of interbedded amphibolite, pyroxene-bearing schist, and leucocratic
pyroxene-bearing plagiogneiss, with migmatized biotite plagiogneiss that
contain boudin-like bodies of amphibolitized two-pyroxene plagiogneiss.
The migmatized biotite plagiogneiss range from quartz diorite to
trondhjemite, whereas the two-pyroxene plagiogniesses are derived from
calk-alkaline diorite and quartz diorite. A U-Pb zircon age for the
biotite plagiogneiss is 2646±30 Ma (Mitrofanov and others, 1985). The
Bumbuger complex comprise two series: (1) an alternating series of
amphibolite two-pyroxene schist and leucocratic pyroxene-bearing gneiss;
(2) alternating fordterite-bearing marble, quartzite,
pyroxene-amphibole, garnet schist, garnet-biotite gniess, and
leucocratic pyroxene-bearing plagiogneiss. Protoliths are metavolcanic
rocks, mainly bimodal basalt and rhyolite with subordinate
metasedimentary rocks (Kozakov, 1986).

Post-tectonic granitoids consist of thin veins and dikes of amphibole
granosyenite, granodiorite and granite with isotopic ages of 1825±5 Ma.
Unconformably overlying Riphean sedimentary units consists of basal
coarse sandstone grading upward to a ridge-forming quartzite,
metasandstone, stromatolitic dolomite, limestone, and
carbonate-sedimentary rocks. K-Ar ages of these rocks are 840 Ma. The
postaccretion units consists of Late Ordovician conglomerate, sandstone,
and coral limestone, Silurian graptolite-bearing shale, Devonian
intermediate to felsic volcanic rocks, sandstone, and siltstone, and
Early Carboniferous shallow marine sedimentary rocks. Stitch complexes
includes the early Paleozoic Baydrag complex and late Paleozoic plutons.
The Baydrag complex consists of biotite plagiogranite and diorite with
isotopic ages of 469 to 551 Ma.

**REFERENCES**: Mitrofanov and others, 1981, 1985; Kozakov, 1986;
Bibikova and others; 1990; Ryazantsev, 1994; Kotov and others, 1995;
Teraoka and others, 1996;, Dergunov and others, 1997; Kozakov and
others, 1997; Takahashi and Delgertsogt, 1997; Takahashi and others,
1998, 1999.

## BZ Bazibai terrane (Metamorphic) (Late Neoproterozoic and Cambrian) (Eastern Sayan)

## 

Occurs in a horst of metamorphic rocks within the less metamorphosed
Vendian-Cambrian volcanic-sedimentary island-arc rocks. Consists of
gneiss, schist, amphibolite, and less marble metamorphosed to
epidote-amphibolite and amphibolite facies. The age of metamorphic rocks
is unknown with interpreted as early Paleozoic.

**REFERENCES**: Nikulchenko and others, 1962; Lebedev and others, 1993;
Berzin, 1995.

## CA Central Angara terrane (Passive continental margin) (Neoproterozoic) (Altai)

Occurs in the central part of the Yenisey Ridge to the east of West
Angara terrane in a belt about 300 km long and ranging up to 50-70 km
wide. Terrane consists of: (1) Late Riphean(?) terrigenous and
terrigenous-carbonate sedimentary rocks metamorphosed to greenschist and
more rarely to epidote-amphibolite facies of the Sukhopit unit that
contains quartz-chlorite-serpentine schist, flysch deposits, limestone,
and dolomite; and (2) unconformably overlapping sedimentary rocks of
Tungusik unit that contains coaly mudstone, flysch, and limestone and
dolomite. These deposits are intruded by calc-alkaline granite of the
Tataka-Ayakhta complex with a isotopic age of 760 Ma and that exhibits a
contact metamorphic halo (Datsenko, 1984). To the north, terrane is
overlapped by the Vendian-Cambrian terrigenous-carbonate deposits.

**REFERENCES**: Khomentovsky and others, 1972; Kornev and others, 1974;
Postel'nikov, 1980.

## Central Aldan Superterrane (Yakutia)

## 

Forms the central part of the Aldan-Stanovoy shield. To the west, is
bounded by the west Aldan composite terrane along the Amga tectonic
melange zone, and to the east is bounded by the East Aldan superterrane
along the Tyrkanda tectonic melange zone. The Central Aldan superterrane
consists of the Nimnyr and Sutam terranes that are separated by the Seim
overthrust with an age of 2.3-1.9 Ga (Gorokhov and others, 1981). The
terranes are dominated by granitoid orthogneiss and lesser sedimentary
rocks (Dook and others, 1986).

**REFERENCES**: Gorokhov and others, 1981; Dook and others, 1986.

## CANM Nimnyr terrane (Granulite-orthogneiss) (Paleoproterozoic) (Yakutia)

## 

> Nimnyr terrane (with areal dimensions of 150 km×200km) occurs in the
> western part of the Central Aldan superterrane. The structural pattern
> of the terrane is defined by a widely-developed granite-gneiss domes.
> The largest is the Timpton dome (with areal dimensions of 175×200 km)
> in the northern part of the terrane (Dook and others, 1986). The cores
> of the domes consist of orthogneiss, including granite-gneiss,
> charnockite- and enderbite-gneiss with amphibolite bodies that
> comprise more than 50 percent of the terrane area. The external parts
> of the domes are composed of a paragneiss complex consisting of two
> rock assemblages: (1) the Kurumkan Group that includes quartzite and
> high-alumina gneiss with lenses of calciphyres and iron quartzite
> (Khil'tova and others, 1988; Dook and others, 1986); and (2) the
> Fedorov Group that contains amphibole, diopside-amphibole, and two
> pyroxene-amphibole plagiogneiss, and rare schist with bands and lenses
> of diopside, phlogopite-diopside rock, and calciphyre. Less common is
> diopside-amphibole and two-pyroxene schist with lenses and beds of
> calc-silicate rocks and calciphyre (Petrova and others, 1975;
> Cherkasov, 1978; Velikoslavinskiy, 1976; Petrova and Smirnova, 1982;
> Beryozkin and Kitsul, 1979). The terrane is metamorphosed to low and
> middle pressure granulite facies.
>
> Sm-Nd isotopic studies of high-alumina gneiss (similar in chemical
> composition to pelite and siltstone) and of interlayered
> biotite-hypersthene plagiogneiss (chemically corresponding to tuff and
> graywacke) indicate that protoliths for the former formed from
> breakdown of the rocks with a Nd age of 2.85-3.06 Ga, while protoliths
> for the latter were derived from the rocks as old as 2.33-2.4 Ga
> (Kovach and others, 1995b). The Fedorov Group resulted from
> metamorphism of protoliths with a model Nd age of 2.1-2.3 Ga (Kovach
> and others, 1995a). The lower age limit of the granulite metamorphism
> of the Kurumkan Group is estimated at 2.3 Ga, whereas that of the
> Fedorov Group is 2.15 Ga. Similar conditions of the granulite
> metamorphism of both groups (Dook and others, 1986) suggest that they
> were most intensely metamorphosed after 2.15 Ga. The upper age limit
> of high-temperature metamorphism is constrained by the emplacement of
> aplite-like granite dated at 1.9±0.15 Ga (Sal'nikova, 1993).
> Diaphthoresis of amphibolite facies rocks and the accompanying
> metasomatism are dated at 1.9-1.8 Ga (Murzaev, 1969; Mikhailov and
> Levchenkov, 1971; Pozharitskaya and others, 1973). Orthogneiss with a
> Nd model age of 2.3-2.5 Ga (Sal'nikova, 1993) contain relics of
> granite-gneiss and tonalite-trondhjemite gneiss which are relatively
> older. The latter are probably relics of the basement rocks upon which
> primary sedimentary rocks accumulated (Dook and others, 1986).
>
> **REFERENCES**: Murzaev, 1969; Mikhailov and Levchenkov, 1971;
> Pozharitskaya and others, 1973; Petrova and others, 1975;
> Velikoslavinskiy, 1976; Cherkasov, 1978; Beryozkin and Kitsul, 1979;
> Petrova and Smirnova, 1982; Dook and others, 1986; Khil'tova and
> others, 1988; Sal'nikova, 1993; Kovach and others, 1995a.

## CAST Sutam terrane (Granulite-paragneiss) (Late Archean) (Yakutia)

## 

> Sutam terrane occurs to the east of the Nimnyr terrane and is shaped
> as a triangle with a base of 100 km and a height of 250 km. The
> terranes are separated by the Seim thrust which is defined by
> intensely layered rodding gneiss of the granulite metamorphic facies.
> Structural pattern of the terrane is defined by linear sublongitudinal
> folds. Most of the terrane consists of paragneiss of the Seim Group,
> the rest consists of granite- and enderbite-gneiss (Khil'tova and
> others, 1988).
>
> The Seim Group consists mainly garnet-biotite gneiss and plagiogneiss,
> sometimes with sillimanite and cordierite, with lesser
> hypersthene-biotite, two-pyroxene, and diopside-amphibole
> plagiogneiss, and rare quartzite, calc- silicate rocks, and
> calciphyres. The rest consists of magnetite quartzite (Khil'tova and
> others, 1988).
>
> Metamorphism of para- and orthogneiss in different parts of the Sutam
> terrane occurred under different conditions (Dook and others, 1986).
> In the Seim block, metamorphism was at middle pressure granulite
> facies, whereas in the Sutam block, metamorphism was at high pressure
> granulite facies. These rocks exhibit the most high-temperature and
> high-pressure granulite facies of the Aldan-Stanovoy shield. Sm/Nd
> data show that parental rocks of paraneisses range in age from 2.5 to
> 2.9 Ga, whereas those of orthogneiss are as old as 3.0 Ga. Their
> synchronous metamorphism occurred after 2.5 Ga. The upper age limit of
> the early granulite metamorphism of the Seim Group rocks is
> constrained by the time of formation of garnet-biotite rodding gneiss
> in the zone of the Seim thrust which is dated at 2.28±0.06 Ga by Rb-Sr
> isotopic studies (Gorokhov and others, 1981). Overlap assemblages
> include Late Riphean and Vendian rocks of the sedimentary cover of the
> North Asian Craton.
>
> **REFERENCES**: Gorokhov and others, 1981; Dook and others, 1986;
> Khil'tova and others, 1988.

## CACG Chogar terrane (Granulite-orthognesiss) (Archean) (Yakutia)

## 

> Chogar terrane (with areal dimensions of 500x100 km) occurs on the
> southeastern margin of the Aldan-Stanovoy shield. Limited K-Ar data
> indicate that the terrane consists mainly of Archean rocks (Karsakov,
> 1983). The terrane consists of two equal-area blocks that are
> separated by a northeast-striking fault. The eastern block consists of
> the Chogar complex that contains hornblende-two-pyroxene,
> garnet-hornblende-two-pyroxene schist and, locally, ultramafic schist,
> and lesser amphibolite and quartzite, iron-quartzite layers, aluminous
> gneiss, and garnet granulite. Metamorphism is sapphirine-quartz
> subfacies of hypersthene-sillimanite facies (Karsakov, 1983). The
> western block is marked by a extensive high-pressure amphibolite
> facies rocks. The dominant rocks are diorite plagiogneiss with lenses
> and bands of amphibole schist with lesser quartzite and aluminous
> gneiss.
>
> **REFERENCES**: Karsakov, 1983.

## CH Chuja terrane (Paragneiss) (Late Archean through Neoproterozoic) (Transbaikalia)

## 

Extends to northeast. In southwest it borders on the North-Asian craton
and Olokit-Delunuran terrane along the overthrust, in the northeast it
borders on the complexes of the Patom sedimentary basin (along the
strike-slip fault fault). To the north, terrane is composed of: (1)
Early Riphean (Bramynsky complex) hypersthene-diopside-
plagioclase-amphibole schist and amphibolite (Neelov, Podkovyrov, 1983)
metamorphosed to amphibolite facies with K-Ar amphibole of 3.5-3.0 Ga;
and (2) Late Archean plagiogneiss with layers of quartzite, marble,
amphibolite, bedded plagiogranite gneiss, and diorite gneiss (Chuysky
series). To the south, the terrane consists of the widespread
metamorphic complex of the Late Archean Ukuchiktinsky series (Manuilova
and others, 1964). Thickness is about 5000 m. The parageneses of
metamorphism consists of the cordierite-andalusite-muscovite,
biotite-muscovite-andalusite, andalusite-garnet-muscovite-biotite and
sillimanite-biotite-muscovite subfacies of the amphibolite facies
(Bolonev and others, 1983). The Paleoproterozoic units of the Chuysky
terrane are: (1) hypersthene granitoids (Tatarnikovsky complex) with
Rb-Sr ages of 2,030 Ma (Sryvtsev and others, 1980); (2) gneiss-like
granite and granodiorite (Chuya complex) with Rb-Sr ages 1,848 Ma
(Makrygina and others, 1993); (3) subalkaline granitoids (Abchadsky
complex) and trachyrhyolite-trachyrhyodacite (Ilovirsky suite) with U-Pb
zircon ages of 1,862 Ma (Neimark and others, 1990); (4) REE metasomatite
with U-Pb zircon ages of 1,007 Ma (Predtechensky and others, 1990); and
(5) dikes and stocks of Early Riphean diabase and gabbro-diabase. The
cratonal and Riphean units are interpreted as accreting to the North
Asian Craton in the Late Riphean with intrusion of stocks and dikes of
granite-porphyry (Yazovsky complex), with U-Pb zircon ages of 730 Ma,
into the Chuysky cratonal terrane (Ivanov and others, 1995).
Post-accretionary units are granite batholiths (Mama complex) with U-Pb
zircon ages of 350-300 Ma (Neimark and others, 1990; Ivanov and others,
1995; U-Pb), REE pegmatite and metasomatite with U-Pb zircon ages of
413, 370, and 320 Ma (Predtechensky and others, 1990).

**REFERENCES**: Manuilova and others, 1964; Sryvtsev and others, 1980;
Bolonev and others, 1983; Neelov, Podkovyrov, 1983; Makrygina and
others, 1993; Neimark and others, 1990; Predtechensky and others, 1990;
Ivanov and others, 1995.

## CHN Cheongjin terrane (Accretionary wedge, type B) (Permian) (Korea)

## 

Consists of serpentinite melange with blocks of gabbro, basalt, schist
and the Permian Tuman Group. Intruded by Early Permian granite of the
Tumangang Complex and the Jurassic Daebu granite.

**REFERENCES**: Geology of Korea, 1993.

## CHR Charysh terrane (Continental margin turbidite) (Cambrian through Devonian) (Northwestern Gorny Altai)

## 

Consists of a basal unit of Cambrian green sand-siltstone flyschoid
sedimentary rocks with units of motley, coarse-grained sandstone,
gravelstone and conglomerate with clasts of red jasper and quartzite
(Charysh and Suetka suites). Upward is an unconformably overlying gray
terrigenous-carbonate sedimentary complex of Ordovician-Silurian age
with organic fossils. The lower part of the complex contains Arenig
(Early Ordovician) graptolites and contains deep-water, fine-terrigenous
flysch that is overlain by shelf deposits and slope deposits. The upper
part is dominated by Late Ordovician and Silurian shallow-water
carbonate reef deposits that comprise a carbonate platform. In the
northeastern part of the terrane, the Silurian deposits occurri in the
graben-like depression of the Kurja-Akimov zone and are overlain by
Early Devonian shallow-water marine carbonate-terrigenous deposits, and
by Early Givetian volcanic rocks of the Altai volcanic belt. The terrane
is intruded by Middle Devonian alkaline and subalkaline granitoids with
a U-Pb age of 381±4 Ma, Late Devonian calc-alkaline and plumasite
granitoids with U-Pb age of 364±8 Ma, and Late Permian-early Triassic
REE granite with a U-Pb age of 251±2 Ma.

**REFERENCES**: Kulkov and Severgina, 1989; Yolkin and others, 1994;
Sennikov and others, 1997; Vladimorov and others, 1997; Iwata and
others, 1997.

## CT Central Taimyr superterrane (Taimyr Peninsula)

## 

Occupies the central part of the Taimyr Peninsula. Extends in a
northeastern direction for 600 km long and ranges up to 70-100 km wide.
Consists mainly of the Chelyuskin, Mamont-Shrenk, Faddey, and Kolosovsky
terranes that were accreted in the Neoproterozoic, and was accreted onto
the North Asian Craton during Vendian obduction. The Central Taimyr
superterrane is overlapped by the Vendian-Carboniferous cover of marine
sedimentary rocks and by the Jurassic-Cenozoic marine and nonmarine
sedimentary rocks.

**REFERENCES**: Zonenshain and others, 1990; Uflyand and others, 1991;
Vernikovsky, 1996, 1997.

## CTC Chelyuskin terrane (Island arc) (Neoproterozoic) (Northeast and Central Taimyr Peninsula)

## 

> Occurs in a northeastern direction 300 km long and ranges up to 100 km
> wide. Consists of two units: (1) a lower unit of serpentinite and
> serpentinite mélange with fragments of Neoproterozoic ophiolite, and
> limestone with spilite and bedded jasper, and black shale; and (2) an
> upper unit of a thick assemblage of Neoproterozoic island arc volcanic
> and sedimentary rocks consisting of tholeiitic basalt, andesite
> basalt, rhyolite, plagiogranite, tuff, sandstone, siltstone, black
> chert, breccia, and dolomite with the Late Riphean stromatolites and
> microphytolites. The subterrane is metamorphosed to greenschist
> facies. The lower unit is interpreted as a Neoproterozoic oceanic
> crust (ophiolite) sequence, and the upper unit is interpreted as a
> Neoproterozoic island arc sequence. The ophiolite forms the Chelyuskin
> and Stanovoy northeast-striking belts. A U-Pb zircon age for
> Chelyuskin plagiogranite is 740[+]{.underline}38 Ma, and a Rb-Sr
> isochron age is 727[+]{.underline}83 Ma. These ages are interpreted as
> the upper age of the Chelyuskin ophiolite. A Sm-Nd model age of
> 850-750 Ma probably is the oldest age (Vernikovsky and others, 1993,
> 1994).
>
> **REFERENCES**: Zonenshain and others, 1990; Uflyand and others, 1991;
> Vernikovsky and others, 1993, 1994, 1996, 1997; Vernikovsky, 1996.

## CTF Faddey terrane (Metamorphic) (Neoproterozoic and older) (Northeastern Taimyr Peninsula)

> Occurs in the central part of North Taimyr and extends in a
> northeastern direction for 100 km long and ranges up to 30-50 km wide.
> Consists chiefly of an isolated structural block that consists of
> high-grade metamorphic (epidote-amphibolite and amphibolite facies)
> metaclastic rocks (plagiogneiss and schist), and metamafic rocks
> transformed into biotite-amphibole schist and amphibolite, with minor
> quartzite, marble, and calciphire. The rocks often exhibit severe
> cataclasis, mylonitization, and diaphthoresis, especially in marginal
> parts. The gneiss contains migmatite-granite and autochthonous granite
> with U-Pb zircon isotopic age of 850 Ma, and a Sm-Nd model age of
> 1.8-1.9 Ga for continental crust (Vernikovsky, 1996). Recent studies
> interpret the terrane as an overthrust slice of the craton (Makhlaev,
> 1978).
>
> **REFERENCES**: Ravich, 1954; Makhlaev, 1978; Zabiyaka and others,
> 1986; Vernikovsky, 1995, 1996, Vernikovsky and others, 1998.

## CTK Kolosovsky terrane (Passive continental margin) (Late Neoproterozoic) (Central Taimyr Peninsula)

## 

> Extends in a northeastern direction for 200 km and ranges up to 30-50
> km wide. Consists of carbonate rocks, limestone, and dolomite with
> Late Riphean stromatolites and microphitolites (Kaban\`kov and others,
> 1978; Bezzubtsev and others, 1978; Yakshin, 1980). A belt of
> volcanogenic rocks consisting of necks and explosion pipes, occurs in
> the central and southwestern parts of the terrane where the limestone
> and dolomite are intruded by the dikelike bodies of gabbro-diabase and
> are overlapped by trachibasalt and basalt tuff, pillow-like and
> rope-like basalt, and rare felsic tuff. This complex of volcanogenic
> rocks may have formed during rifting of a Late Riphean-Vendian active
> continent margin. The relation of these carbonates with
> volcanic-sedimentary and crystalline units of the Chelyuskin and
> Mamont-Shrenk terranes is conjectural because of lack of reliable
> observations of relationships. Either tectonic contact occur, or the
> carbonate rocks are separated by concealed exposure from the other
> complexes. Terrane is interpreted as a fragment of a passive
> continental margin, probably the North Asian Craton (Kaban\`kov and
> others, 1978; Uflyand and others, 1991), and was accreted in the
> Neoproterozoic with the other terranes of the Central Taimyr
> superterrane.
>
> **REFERENCES**: Kaban\`kov and others, 1978; Bezzubtsev and others,
> 1978; Yakshin, 1980; Uflyand and others, 1991; Vernikovsky, 1996.

## CTM Mamont terrane (Metamorphic) Mesoproterozoic and Neoproterozoic) (Taimyr Peninsula)

## 

> Occurs in the central part of Taimyr between the Mamont and Shrenk
> Rivers with dimensions of about 50 x 50 km. Consists of
> biotite-sillimanite and garnet-biotite gneiss and schist; and
> metamafic rocks transformed into biotite-amphibole schist and
> amphibolite with bodies of amphibolite gabbros and granitoids.
> Granitoids comprises about 50% of the terrane and forms elongated
> lens, plates, and massifs lying concordantly with strike of folded
> structures, with sizes of tens to hundreds km^2^. Granitoids are
> mainly two-mica and biotite porphyry granite of normal and subalkaline
> potassium-sodium series (Ravich, Chaika, 1962; Makhlaev, 1988; Zakarov
> and others, 1993; Vernikovsky, 1996). S-type origin is suggested by a
> autochthonous bedding, ratio of petrogenic components, REE
> inheritance, and frequent garnet. A Th-U-Pb method zircon age of about
> 900 Ma is exhibited by the Shrenk granite using Cameca IMS 1270
> ion-microprobe located at the Swedish Museum of Natural History,
> Stockholm (Pease and others, 2001). Two interpretations exist for the
> terrane. (1) Terrane may be uplifted Archean and Lower Proterozoic
> North Asian Craton basement (Bezzubtsev, 1981; Bezzubtsev and others,
> 1986; Zabiyaka and others, 1986). Or (2) terrane may be high-grade
> metamorphosed rocks and granitoids tectonically combined with other
> terranes (island-arc, back-arc, and carbonate) of the Central Taimyr
> superterrane.
>
> **REFERENCES**: Bezzubtsev, 1981; Bezzubtsev and others, 1986;
> Zabiyaka and others, 1986; Ravich, Chaika, 1962; Makhlaev, 1988;
> Zakarov and others, 1993; Vernikovsky, 1996; Pease and others, 2001.

## DB Dibinsky terrane (Accretionary wedge, Type A) (Late Neoproterozoic) (Eastern Sayan, Mongolia)

## 

Consists of Riphean sedimentary and sedimentary-volcanogenic formations
of the Dibinsky sequence that contains predominantly rhythmically
layered sedimentary rocks mainly siltstone with sandstone, carbonate
rocks and conglomerate with gradational layering. Olistostrome horizons
occur with serpentinite olistoliths. Diabase and gabbro-diabase form
both subvolcanic bodies (sills or dikes) (Belichenko and others, 1988).
Terrane is overlapped by the Vendian-Cambrian carbonate-terrigenous
rocks.

**REFERENCES**: Belichenko and others, 1988.

## DL Daldyn terrane (Granulite-orthogneiss) (Middle Archean) (Yakutia)

## 

Consists mainly of enderbite and mafic schist of the Daldyn and Late
Anabar Groups with lesser metasedimentary rocks inncluding quartzite and
carbonate rocks. Enderbite derived from tonalite and quartz diorite.
Two-pyroxene and hypersthene mafic schist and enderbite-schist form two
bands in the central part of the terrane, and geochemically correspond
to tholeiite basalt. Igneous rocks of the terrane are divided into
calc-alkalic, alkalic, and subalkalic series, and are comparable to
island arc volcanic rocks (Rosen and others, 1994). Terrane is multiply
deformed mappable, linear, compressed, northwest-trending folds with
steeply dipping hinges and axial surfaces. Enderbite of the Daldyn
terrane exhibits a U-Pb concordia zircon age of 3.2+0.32 Ga. A Sm-Nd
isochron age of 3.1+0.8 Ga exists for mafic granulite (Rosen and others,
1994). The data suggest an age of 3.1 Ga for the protolith of the
terrane. Terrane underwent intense metamorphism of granulite facies and
to the north exhibits hypersthene-sillimanite zone of granulite facies
(Vishnevskiy, 1978; Lutz and Oxman, 1990). Granulite metamorphism and
synchronous deformation exhibit a U-Pb discordia zircon age of 2.8 Ga
(Rosen and others, 1994). Terrane is bounded by the Kotuykan and
Billyakh melange zones to the west and east, respectively, and is cut by
the Major Anabar strike-slip fault containing pseudotachylite, mylonite,
and cataclasite. Terrane can be traced to the north and south beneath
sedimentary cover by geophysical data.

**REFERENCES**: Vishnevskiy, 1978; Lutz and Oxman, 1990; Rosen and
others, 1994.

## DN Dongwuzhumuqin-Nuhetdavaa terrane (Island arc) (Cambrian through Middle Devonian) (Northeastern China, Mongolia)

Consists of the Dongujmqin terrane in China and the Nuhetdavaa terrane
in Mongolia. In northeast China, consists of: (1) Early Cambrian
crystalline limestone intercalated with shale with archaeocyatha and
trilobite fragments; (2) Middle and Late Ordovician andesite, low-grade,
metamorphosed fine-grained clastic rocks intercalted with limestone with
trilobites, brachipods and corals; (3) Late Silurian low-grade,
metamorphosed sandstone, slate and intercalated lenses of limestone with
brachipods; And (4) Early and Middle Devonian sandstone, siltstone and
fine sandstone intercalated with lenses of limestone, volcanic rocks,
tuff and Late Devonian clastic rocks, slate, mud rocks, and siltstone
with brachipods and corals. Terrane is unconformably overlain by Early
Carboniferous andesite, tuff and fossil plant-bearing terrestrial
clastic rocks, and by Early Permian andesite, tuffaceous sandstone.
Terrane is intruded by Late Carboniferous calcic-alkaline granite.

**REFERENCES:** Bureau of Geology and Mineral Resources of Xinjiang
Uygur Aut. Reg.(Xinjiang GMRB), 1990; Tang Kedong, 1990; Xie Tonglun,
1980.

In eastern Mongolia, consists of: (1) middle to late Riphean (?) gneiss,
schist, stromatolite marble, and limestone; (2) Early to Middle Cambrian
sandstone and siltstone, and minor conglomerate and olistostrome, (3)
Middle to Late Ordovician sandstone, siltstone, and phyllite, minor
conglomerate and limestone with corals; (4) Silurian sandstone,
siltstone, and argillite, and minor coral limestone that are
metamorphosed to greenschist facies and contain deformed lenses of
serpentinite and gabbro; (5) Early to Middle Devonian thick sandstone,
siltstone, and argillite, and minor basalt, andesite, tuff,
conglomerate, and limestone with brachiopods and corals. Terrane is
intruded by Silurian granite and granodiorite, and by minor quartz
diorite with K-Ar isotopic ages of 419-435Ma. Terrane is overlain by
Early Carboniferous shallow-marine sedimentary rock, Middle to Late
Carboniferous and Permian subalkalic and alkalic volcanic and
volcaniclastic rock, and is stitched by Middle to Late Carboniferous and
Permian granite and leucogranite, and by Triassic and Early Jurassic
rare metal granite.

**REFERENCES:** Geology of Mongolian People's Republic, 1973; Tang,
1990; Hsu and others, 1991, Badarch and Orolmaa, 1998.

## DR Derba terrane (Passive continental margin) (Late Neoproterozoic) (Eastern Sayan)

## 

Consists of tectonic wedges and sheets composed of rocks of various ages
and environments. Generally consists of three sequences, from bottom to
top. (1) Alygzher suite of biotite, biotite-amphibole,
biotite-amphibole-pyroxene gneiss and schist with garnet, cordierite,
sillimanite, and graphite and lesser graphite-bearing quarztite, marble
and calciphyres. (2) Derba suite of graphite-bearing marble and
quarztite with subordinate gneiss and schist. And (3) Zhaima suite of
graphite-quartz and quartz-mica schist, quarztite, and calciphyres
interbedded with marble-like limestone. Locally, the suite consists of
alternating thin layers. A total thickness of the three sequences is 8-9
km. Sequences are apparently overlain by carbon-rich shale-carbonate
deposits that are exposed along bounding faults and resemble Late
pre-Cambrian accretionary units. The terrane is interpreted as
metamorphosed sedimentary rocks of the North Siberian passive
continental margin. Terrane exhibits a strongly compressed
nappe-imbricated structure in which individual sheets have a linear
orientation and steep layering. In the central parts of the terrane the
rocks are metamorphosed to amphibolite facies. The periphery exhibits
epidote-amphibolite and greenschist metamorphism, with several tectonic
lenses of strongly metamorphosed rocks. Pre-Vendian and
Camrian-Ordpvician(?) collisional granite occur widely distributed in
the southeastern part of the train with a majority of K-Ar biotite ages
of 417-542 Ma for granite. The central area is intruded by a diagonal
belt of Early Devonian rift-related granitoids. The Riphean(?) Derba
terrane is separated from the ancient blocks of the North-Asian Craton
Margin by the Main strike-slip fault of Eastern Sayan.

**REFERENCES**: Khomentovsky, 1957; Polkanov and Obruchev, 1964; Berzin,
1967; Parfyonov, 1967; Sez'ko, 1982.

## DZ Dzhida terrane (Island arc) (Late Neoproterozoic and Early Cambrian) (Transbaikalia, Mongolia)

## 

In Mongolia, terrane occurs southeast of Hovsgul lake, north of Hangay
strike-slip fault and extends to northeast for 250 km and ranges up 170
km wide. Consists of five thrust panels of late Precambrian and early
Paleozoic rocks composed of the following two groups of rock. (1)
Dismembered Precambrian ophiolite containing dunite, harzburgite,
sheeted dike, boninite lava and tholeiitic basalt. And (2) Vendian to
Early-Cambrian volcanic rocks subdivided into high titanium subalkalic
basalt and calc-alkalic basalt-andesite-rhyolite series. The former are
interpreted as seamount volcanic rocks and later are interpreted as
oceanic island arc volcanic rocks (Al\'mukhmedov and others, 1996,
Tomurhuu, 1999). Volcanic rocks of all thrust panels are depositionally
overlain by Cambrian(?) calcarenite-terrigenous rocks, tuffaceous flysch
with archaeocyatha, and local olistostrome. In the island arc volcanic
rocks are small bodies of gabbro and palgiogranite with K-Ar ages of 540
Ma (I\'lin, 1982). Post accretionary assemblages are Middle Ordovician
S- type granite and Silurian marine molasse.

**REFERENCES:** I\'lin, 1982, Kheraskova and others, 1987, Tomurtogoo,
1989, 1997, Al\'mukhmedov and others, 1996, Tomurhuu, 1999.

In Transbaikalia, terrane extends in a sublatitudinal direction for
nearly for 300 km and ranges up to 150 km wide. Consists of five thrust
panels of Vendian-Cambrian rocks. These thrust panels consists chiefly
of units similar to those described above for Mongolia. The carbonate
and silicic-greywacke sedimentary rocks with Early Cambrian fauna are
interpreted as seamounts (Belichenko, 1977, 1996; Kheraskova and others,
1987). Olistostrome horizons also occur. Intruding these units are small
and later large massifs of gabbro-plagiogranite (Nashituy complex) that
form the base of the island arc. Ophiolites occur in the lowermost part
of the terrane and consist of Late Riphean(?) restite alpine type
ultramafic rocks and basalt of mid-oceanic type. They are commonly
strongly serpentinised and deformed. The tholeiitic metabasalt is
characterised by extremely low K/Na ratios, are somewhat depleted in
SiO~2~. CaO dominates over MgO with moderate TiO~2~. Compositions
correspond to of spreading zone basalt.

Overlapping units are flyshoid sedimentary rocks of the widespread Late
Cambrian to Devonian Dzhida suite that contain fragments of graptolites,
bryozoans (Almukhamedov and others, 1996). Younger granitoids in
Mongolia have a K-Ar isotopic age of 542 Ma (Middle Ordovician) (Il'in,
1982), to 430 Ma (Distanova, 1975). The upper part of the overlapping
units consists of Devonian variegated molasses with siliceous volcanic
rocks (Khurliksky suite). All sedimentary rocks of the terrane are
intruded by K-series, S-type granitoids with isotopic ages of 380-320 Ma
(Il'in, 1982).

**REFERENCES**: Belichenko, 1969; 1977; Distanova, 1975; I\'lin, 1982;
Kheraskova and others, 1987; Tomurtogoo, 1989, 1997; Al\'mukhmedov and
others, 1996; Belichenko and others, 1996; Tomurhuu, 1999.

## DZA Dzhagdy terrane (Accretionary wedge, type B) (Late Carboniferous and Permian) (Southern Russian Far East)

Consists of Late Pennsylvanian(?) and Early Permian, intensly-deformed,
phyllite, chert, metabasalt, microquartzite, and limestone lenses
(Dzheskogon, Nekter, and Bochagor suites), and late Paleozoic(?) gabbro
and amphibolite. The limestone contains an Early Permian Tethyan fauna
(corals, fusulinids). Six stages of deformations and associated
greenschist facies are recognized with begining stage being the most
intensive with formation of recumbent and overturned isoclinal folds and
associated thrust faults with northern vergence.

**REFERENCES**: Kirillova and Turbin, 1979; Natal\'in and others, 1985;
Martynyuk and others, 1990; Natal\'in and Popeko, 1991; Natal\'in, 1993;
Popeko, Natal\'in, and others, 1993, Krasnyi and others, 1996.

## DZE Dzhebash terrane (Accretionary wedge, type A) (Late Neoproterozoic and Early Cambrian) (Northwestern Sayan)

## 

Consists of the Dzhebash volcanic-sedimentary series that are
metamorphosed to greenschist and epidote-amphibolite facies, and
contains the Tebin (lower) and Urten (upper) suites. The Tebin suite
consists of monotonous paraschist derived from rhythmically-layered
sandstone, claystone, and calcareous sedimentary rocks. Metavolcanic
rocks from 10-30 m thick paraschist packages in the lower part, and
dominate the upper part of the Urten suite. The volcanogenic rocks
consists of tuff, tuffaceous sandstone, basalt, and andesite, are
metamorphosed to chlorite-albite-epidote-actinolite schist and
metaporphyries. Also occurring in the Dzhebash seriesthere are beds and
lenses of marble-like limestone; the thickest horizon of carbonate rocks
varies up to 50-150 m thick and occurs below the base of the Urten
suite. Horizons limestone lenses are interpreted as forming from
submarine landslides. Also occurring are interlayered micaceous
quarztite, quartz-hematite schist, and piedmontite quartzites. Peak
metamorphism likely was in the middle Paleozoic metamorphism most
clearly displayed in the northeastern and southwestern extremities of
the terrane. A K-Ar biotite isotopic age is 364 Ma, and a K-Ar muscovite
isotopic age is 356 Ma for mica from an ultrametamorphosed
granite-gneiss in the Dzhebash series. Terrane is intruded by Early
Devonian(?) gabbro and gabbro-diorite of the Bichebalyk complex, diorite
and granodiorite of the Bolshoi Porog complex, and granite and
granosyenite of the Dzhoi complex. Overlapping deposits are Devonian
continental volcanic-sedimentary rocks, which occur in small,
graben-like depressions along the faults that bound the terrane. The age
of the Dzhebash suite is unclear; the volcanic-flysch unit may have
formed in the Vendian-Early Cambrian in an accretionary wedge or at the
front of a growing island arc.The Dzhebash, and related Borus and Amil
terranes form a system of large tectonic lenses that are tectonically
linked to the North-Sayan island-arc terrane.

**REFERENCES**: Zonenshain, 1963; Korobeinikov and Isakov, 1965;
Kazakov, 1967; Klyarovsky, 1972; Sobolev and Dobretsov, 1977; Kheraskov,
1979; Berzin, 1995; Zaltsman and others, 1996.

## ED Edren terrane (Island arc) (Devonian and Early Carboniferous) (Southwestern Mongolia)

## 

Occurs south of Transaltay fault and forms narrow, northwest trending
block in southwestern Mongolia. Consists of: (1) Early Devonian basalt,
andesite, tuff, radiolarian chert, sandstone, siltstone and lenses of
limestone, with brachiopods; (2) Middle to Late Devonian interbedded
tuff, conglomerate, sandstone, siltstone, chert; and (3) Early
Carboniferous basalt, andesite, tuff, conglomerate, sandstone with
lenses of limestone with brachiopods and bryozoans. Trace element data
from Devonian volcanic rocks plots indicate formation in a volcanic arc
and are most similar to the New Hebrides arc patterns. Terrane overlain
by Middle Carboniferous conglomerate, sandstone, siltstone, and
limestone with brachiopods, and Middle to Late Carboniferous and Early
Permian subalkalic volcanic rocks. Postaccretion granitic rocks consists
of Early to Middle Carboniferous diorite, granodiorite, granite, and
Early Permian leucogranite. Terrane is interpreted as a fragment of an
island arc that formed on oceanic crust or an accretionary wedge.

**REFERENCES**: Tikhonov, 1982; Gordienko, 1987; Ruzentsev and others,
1987; Suetenko and others, 1988; Yarmolyuk and Badarch, 1990; Lamb and
Badarch, 2001.

## East Aldan superterrane (Yakutia)

## 

The East Aldan superterrane, with approximate dimensins of 450 by 500
km, occurs east of the Central Aldan superterrane, and includes the
Uchur granulite-paragneiss terrane and the Batomga granite-greenstone
composite terrane.

## EUC Uchur terrane (granulite-paragneiss) (Paleoproterozoic) (Yakutia)

## 

> Occurs mostly in Yakutia and is defined by a structural pattern
> consisting of granite-gneiss domes measuring with average diameters of
> 150 km. The cores of the domes consist of granite-gneiss,
> charnockite-gneiss, and enderbite-gneiss. The paragneiss complex
> includes two rock assemblages: (1) garnet-biotite plagiogneiss
> interlayered with calc-silicate rocks, quartzites, sillimanite- and
> cordierite-bearing gneiss, and hypersthene, diopside, and two-pyroxene
> plagiogneiss, (2) hypersthene, hypersthene-diopside, and
> hypersthene-diopside-amphibole plagiogneiss with the
> hypersthene-bearing rocks prevailing., along with bands and lenses of
> hypersthene-amphibole, two-pyroxene-amphibole, diopside-amphibole
> schist, and calc-silicate and diopside granofels. Also occurring are
> thin sheets of garnet-biotite, garnet-hypersthene-biotite
> plagiogneiss, and gneiss. Metamorphic conditions were extensively
> studied by V.I. Kitsul (Dook and others, 1986). The grade of
> metamorphism is high-pressure granulite facies with average
> temperature of 780-820^0^ C, pressures of 7 kbar. Sm-Nd isotopic data
> indicate that paragneiss is derived from the rocks of 2.6-2.1 Ga age,
> and that metamorphism probably occurred after 2.1 Ga. The end of
> high-temperature metamorphism is estimated at 2.0-1.8 Ga based on
> Pb-Pb zircon isotopic age for charnockites in the Emelyali pluton.
>
> **REFERENCES**: Dook and others, 1986; Glukhovskiy and others, 1993.

## EBT Batomga composite terrane (Granite-greenstone) (Late Archean) (Yakutia)

> Occurs on the northeastern margin of the Aldan-Stanovoy shield with
> average dimensions of 200 by 100 km. Forms a basement uplift covered
> by sedimentary rocks of the Siberian Platform. Ulkan fault forms
> western boundary and is traced under the platform by intense positive
> linear magnetic anomalies. Interpreted as an Archean
> granite-greenstone terrane though reliable age determinations are
> lacking now. Dominated by tonalite-trondhjemite orthogneiss (Batomga
> complex) with thin bodies of mafic schist, along with lesser granite
> gneiss and granite. Metamorphosed to amphibolite facies. Mafic rocks
> locally include parageneses metamorphosed to granulite facies.
>
> Batomga complex occurs in five blocks (subterranes) that are separated
> by four northeast-striking zones that range up to 150 km long and 10
> to 20 km thick. Within blastomylonite zones are tectonic greenstone
> wedges of volcanic-sedimentary rocks (Chumikan complex) that occur as
> biotite, two-mica, sometimes garnet- and fibrolite-bearing,
> microgneiss, metasandstone, quartzite, and tremolite marble, as well
> as fine-grained amphibole schist and amphibolite that are interpreted
> as metamorphosed tholeiitic basalt. Locally in the Batomga complex are
> two tectonic blocks of granulite facies rocks (Omninsk complex), about
> 40x50 km in size, that occur near the blastomylonite zones, and are
> dominated by garnet-biotite plagiogneiss and gneiss (with local
> sillimanite), marble, calciphyres, and calc-silicate rocks, with
> lesser orthopyroxene-amphibole, and two-pyroxene-amphibole schist.
>
> The Batomga granite-greenstone, Uchur granulite-paragneiss terranes,
> and intervening Ulkan fault are overlain by volcanic-sedimentary rocks
> of the Ulkan Series with rhyolite with U-Pb zircon ages of 1.7-1.8 Ga
> (Neimark and others, 1992, Tugarinov and others, 1965) with intruding
> granites and hornblende syenites with U-Pb zircon ages of 1.7-1.72 Ga
> (Neimark and others, 1992).
>
> **REFERENCES**: Tugarinov and others, 1965; Khil'tova and others,
> 1988; Petrov, 1990; Neimark and others, 1992; Fed'kin and others,
> 1996.

## ER Eravna terrane (Island arc) (Late Neoproterozoic and Early Cambrian) (Transbaikalia)

## 

Occurs in the central part of western Transbaikalia. It extends in the
submeridional direction over 400 km with a width of about 250 km. Mostly
separated from adjacent terranes by overlapping assemblages. Sedimentary
rocks of the Eravna terrane also form scattered, variable-size xenoliths
granitoids of the vast Barguzin-Vitim batholith. This relation hampers
determing the original boundaries of the terrane. Consists of
Vendian-Cambrian volcanic-sedimentary rocks of the Oldyndisnky suite.
The volcanogenic part is predominantly rhyolite-dacite, dacite,
andesite-dacite, and rhyolite volcanic rocks, with minor diabase and
basalt porphyries. Pyroclastic units predominate over flows. Also
occurring are widespread, subvolcanic, stock-like and sill-like bodies
of lava breccia, and lesser dikes and sills of diabase and andesite
porphyries. The volcanogenic rocks vary continuous from andesite-basalt
to rhyolite. The Oldyndinsky suite contains SEDEX deposits of lead-zinc,
pyrite-siderite, sulphide-hematite, and hematite. The sedimentary part
of the suite consists mainly of limestone with minor
carbonaceous-carbonate shale, siltstone, and sandstone, locally with
reefs, bioherms, and biostromes containing archaeocyatheans, trilobites,
algae. The Oldyndinsky suite is overlapped by sandstone and shale Late
Cambrian-Ordovician Khimogildinsky suite and molasse and variegated
sedimentary rocks of the Devonian(?) Istashinsky suite.

**REFERENCES**: Belichenko, 1969, 1977; Vasiliev, 1977; Kremenetskiy,
1982.

## GA Govi Altai terrane (Continental-margin turbidite) (Cambrian through Devonian) (Mongolia)

## 

Forms a narrow, up to 50km wide, and about 1800 km long belt in southern
Mongolia. Consists of: (1) Cambrian(?) to Early Ordovician sandstone and
argillite, minor volcanic rocks, and limestone; (2) Early to Middle
Ordovician sandstone and argillite, minor conglomerate, and limestone
with brachiopods; (3) Silurian sandstone, argillite, minor limestone,
olistostome, conglomerate, and volcanic and plutonic rocks; (4) Early to
Middle Devonian conglomerate, sandstone, siltstone, coral-bearing
limestone, sparse pillow basalt, and andesite, tuff; (5) unconformably
overlying Middle to Late Devonian conglomerate, sandstone, argillite,
sparse and limestone, and (6) Early Carboniferous conglomerate,
sandstone, siltstone with marine fauna. Preaccretionary granite rocks
include Late Silurian leucogranite and Middle Devonian diorite and
granodiorite. Terrane is overlain by Middle to Late Carboniferous and
Early Permian, mainly bimodal volcanic rocks and volcaniclastic rocks,
and Middle to Late Triassic, and Late Jurassic to Early Cretaceous
subalkalic and calc-alkalic volcanic rocks. Terrane is interpreted as
early a Paleozoic continental margin turbidite basin that formed
adjacent to an inactive and eroded island arc.

**REFERENCES**: Badarch, 1988, Tsukernik and others, 1986, Ruzhentsev
and others, 1987, Badarch and Orolmaa, 1998, Lamb and Badarch, 1997,
2001.

## GG Gargan terrane (Cratonal) (Archean and Paleoproterozoic) (North Huvsgol, Mongolia, Eastern Sayan)

## 

In Mongolia, occurs north of the Hovsgol lake and forms small (50 by 70
km) block between the Hug and Hamar Davaa terranes Consists of Archean
and Paleoproterozoic granite-gneiss, amphibolite, schist, marble and
quartzite overlain by Vendian to Early Cambrian shallow-marine
limestone, and intruded by early Paleozoic granite. Terrane is
interpreted as a cratonal block that accreted to the Siberian continent
in the Vendian.

**REFERENCES:** Belichenko and others, 1988; Fedrovskii and others,
1995.

Terrane occurs in the southeastern part of Eastern Sayan region, and
extends along a southwest direction for over 50 km and ranges up to 20
km wide. Terrane is overthrust onto adjacentg terranes. Consists mainly
of plagiogranite gneiss with inclusions of gneiss, amphibolite, and
schist. Rb-Sr isotopoic age of plagiogranite gneiss is 3153±57 Ma. U-Pb
zircon ages group at about 2 Ga and 460 Ma. The latter are interpreted
as the result of early Paleozoic dome formation. The early Precambrian
formations are overlapped by the Riphean carbonate and
terrigenous-carbonate sedimentary rocks (Irkutny suite). The
amalgamation of the Gargan, Dibinsky, Ilchirsky, and Hug terranes
resulted in formation of the basement of the Tuva-Mongolian
microcontinent which was later overlapped by the Vendian-Cambrian
sedimentary cover composed of carbonate and terrigenous-carbonate
sedimentary rocks (Bokson series). The Sumsunursky tonalites with Rb-Sr
and U-Pb isotopic ages of 790 Ma intrude the crystalline rocks of the
microcontinent basement and the overlapping Riphean carbonate
sedimentary rocks.

**REFERENCES**: Belichenko and others, 1988, 1999; Fedorovskii and
others, 1995; Aktanov and others, 1999;Khain and others, 1999;
Kuzmichev, 1999.

## GL Galam terrane (Accretionary wedge, type B) (Cambrian through Early Carboniferous) (Southern Russian Far East)

## 

Consists chiefly of poorly-studied Paleozoic deposits. To the northwest
the Galam terrane is separated from the Baladek terrane by the Uligdan
dextral strike-slip fault; to the southeast terrane is bounded by the
Tugur fault.

In the northwestern part of the terrane, Paleozoic rocks form an
imbricate stack of thrust sheets that consist of three different
age-rock associations: (1) coherently bedded turbidite; (2) basalt,
ribbon chert, and siliceous shale; and (3) olistostrome. The
olistostromes locally contain inclusions of anorthosite and granitic
rocks similar to those in the Baladek terrane. Each age-rock association
occurs in various tectonic slices and sheets separated by ductile faults
that occur parallel to bedding of internal parts of the sheets. The
internal parts of the sheets are relatively weakly deformed. The
following sedimentary rocks in the terrane range from Cambrian to
Permian. (1) Cambrian and Ordovician limestone with archaeocyaths,
trilobites, inarticulate brachiopods, and algae occur as olistoliths in
a flysch matrix. Siberian-type Archaeocyaths differ from in the Bureya
superterrane. Thick Silurian sequences contain corals and brachiopods
typical of the Okhotsk province. (2) Early and Middle Devonian flora
oocur in the turbidites. The Middle and Late Devonian turbidites contain
poorly preserved bryozoans and crinoids, and poorly preserved
radiolarians sparese chert with post-Early Devonian age. (3) Early
Carboniferous turbidites contain bryozoans, brachiopods, crinoids, and
flora. And (4) Late Permian units contain abundant flora, and
Carboniferous and Permian flora belong to the Angara
paleophytogeographic province. Paleontological data suggest turbidite
rejuvenation to the southeast.

The structure of the southeastern Galam terrane is similar to the
northwestern part and the terrane consists mainly of Middle Devonian and
Early Carboniferous turbidites and olistostromes, and Silurian and Early
Devonian units are absent. Local oceanic chert and mafic volcanic rocks
occur in individual tectonic slices and sheets. Middle and Late Devonian
olistostromes contain inclusions of granitic rocks and limestone with
Cambrian archaeocyaths and trilobites. The matrix in the olistostrome
deposits is mainly greywacke, siltstone, and shale. The Devonian units
contain corals, bryozoans, brachiopods (Verkhoyansk type), and flora,
and the Early Carboniferous units contain foraminifers. Most of the
Galam terrane is overlain by the Late Triassic-Jurassic overlap
assemblage deposits of the Torom sedimentary basin, and the Cretaceous
Khingan-Okhotsk volcanic-plutonic belt. Terrane is interpreted as an
accretionary wedge complex that was tectonically linked to a Devonian
volcanic arc which is partly preserved in the Okhotsk terrane. The
current position is the result of dextral strike-slip faulting that
occurred in the late Mesozoic.

**REFERENCES**: Karaulov, 1966; Gorekhov and Karaulov, 1969; Kozlovskiy,
1988; Natal'in, 1991; Natal'in and Popeko, 1991; Popeko and others,
1993; Krasnyi and others, 1996.

## Galam terrane (Accretionary wedge -- type A) (Cambrian through Early Carboniferous) (Northern part of the Russian Southeast)

Consists of an imbricate stack of thrust sheets of Cambrian, Ordovician,
Silurian, Missisipian and Permian sedimentary and mafic volcanic rocks
three age-rock associations: (1) coherently-bedded turbidite; (2)
basalt, ribbon chert, and siliceous shale; (3) olistostrome; and (4) and
gabbro, diorite, and plagiogranite with K-Ar isotopic ages of 388-317 Ma
that intrude the Silurian deposits. Each age-rock association occurs in
various tectonic slices and sheets that are separated by ductile faults
that occur parallel to the bedding in sheets. Internal parts of the
sheets are comparatively weakly deformed. The Early Cambrian, Silurian,
Early-Middle Devonian sedimentary rocks contain faunal assemblages that
differ from the assemblages in other parts of the Mongol-Okhotsk belt
and in adjacent units to the south. Early Cambrian archaeocyatheans are
similar to those in Siberian palaeobiogeographic province, and Silurian
and Early-Middle Devonian brachiopods are similar to those in the
Okhotsk terrane and Verkhoyansk fold belt. Overlapping sedimentary
assemblages are: (1) Late Triassic-Jurassic shallow-marine terrigenous
deposits of the Torom sedimentary basin; (2) Late Jurassic and Early
Cretaceous terrigenous deposits of the Uda sedimentary basin; (3)
Cretaceous bimodal volcanic rocks of the Khingan-Okhotsk
volcanic-plutonic belt; and (4) the stitching Cretaceous granitoids of
the Khingan-Okhotsk volcanic-plutonic belt. Right-lateral strike-slip
displacement occured along the Uligdan fault which bounds Galam terrane
on the north.

**REFERENCES**: Karaulov, 1966; Gorekhov and Karaulov, 1969; Kozlovskiy,
1988; Natal'in, 1991; Natal'in and Popeko, 1991; Popeko and others,
1993; Krasnyi and others, 1996.

## GN Gonzha terrane (Passive continental margin) (Late Archean(?), Paleoproterozoic(?), and early Paleozoic) (Southern Russian Far East)

## 

Contains of two basement series: (1) Late Archean(?) metamorphic rocks
consisting of biotite, hornblende, garnet-biotite, pyroxene-hornblende
gneiss and schist (Gonzhinsk series) that are metamorphosed to
amphibolite facies; (2) Paleoproterozoic(?) sedimentary rocks that
contain lenses of mafic rocks (Chalovsk series), both metamorphosed to
greenschist facies; (3) early Paleozoic(?) cataclastic and foliated
granitic rocks and plagiogranite occur with the metamorphic rocks; and
Devonian and Early Carboniferous shallow-marine clastic deposits with
limestone layers (Bolsheneversk, Imchansk, Oldoisk, and Tiparinsk
suites) that are faulted against the metamorphic rocks. The first two
units also contain lenses of ultramafic rock. Ages of metamorphic rocks
are based on regional correlations. Post-amalgamation Jurassic
shallow-marine marine and nonmarine clastic rocks overly and link the
Gonzha, Oldoi, and Gar terranes. Early Cretaceous volcanic and granitic
rocks of the Umlekan-Ogodzhin belt overlie or intrude the Gonzha, Oldoi,
Mamyn, and Turan terranes.

**REFERENCES**: Krasny, 1966; Shilo, 1982; Volsky, 1983; Kozlovsky,
1988.

## GR Gar terrane (Accretionary wedge, type B) (Proterozoic?) (Southern Russian Far East)

## 

Consists chiefly of greenstone, metatuff, metasandstone, quartzite,
phyllite, limestone, lenses of ultramafic rocks, and gabbro that are
intensively deformed into schistose melange. May be Proterozoic(?) age,
but only age constraint is clasts of ultramafic rocks and other units of
the Gar terrane in overlapping Jurassic deposits. Terrane
characteristically overlapped by a thick assemblage of Late Triassic
clastic rocks (Kalakhtinsk, Malokalakhinsk, Naptarginsk, and Neupokoevs
suites) with abundant Monotis and Halobia, and is also overlapped by
Jurassic sedimentary rocks (Uralovskinsk, Uskalinsk, Ayaksk, Depsk, and
Molchanovsk suites) that also overly the Oldoi and Gonzha terranes.

**REFERENCE**: Krasny, 1966.

## GS Gurvansayhan terrane (Island arc) (Silurian through Early Carboniferous) (Southern Mongolia)

## 

Occurs in central part of southern Mongolia, south of Mandalovoo and
Mandah terranes, and consists of at least four allochtonous sequences
composed of Silurian to Early Carboniferous volcanic and volcaniclastic
sedimentary rocks. Terrane typically consists of: (1) Pre-Late Silurian,
dismembered ophiolite and serpentinite melange; (2) Late Silurian to
Early Devonian tholeiitic pillow basalt and basalt-andesite, red chert,
volcaniclastic sandstone, and siltstone; (3) Middle to Late Devonian
volcaniclastic sandstone, siltstone, ash tuff and argillite, minor
chert, conglomerate and olistostrome; and (4) Early Carboniferous
conglomerate, sandstone and siltstone with olistostromes. Early Devonian
basalt is similar to the Grenada basalt in the Lesser Antilles arc on
the basis of major and trace element data. Terrane is overlain by Middle
to Late Carboniferous and Permian volcanic and sedimentary rocks and by
Jurassic continental deposits. Terrane is interpreted as a fragment of a
Silurian to Early Carboniferous island arc and fore-arc and back-arc
basin.

**REFERENCES**: Suetenko, 1973; Zonenshain and others, 1975; Ruzhentsev
and others, 1985, 1987; Eenjin, 1983; Badarch, 1990; Badarch and
Orolmaa, 1998; Lamb and Badarch, 1997, 2001.

## HD Hangay-Dauria terrane (Accretionary wedge, type A) (Silurian through Late Carboniferous) (Transbaikalia, Mongolia)

## 

Consists of two uneaqual parts, the larger extending from Central
Mongolia to the northeast into the eastern Transbaikalia region and
forms a band that is 900 km long and varies from 100 to 120 km wide. A
smaller part, that has dimensions of 450 by 150 km, occurs in central
Mongolia, and is separated from the larger part by a narrow zone of the
Onon terrane. Generally, the terrane boundaries are not clear. Only in
the northeast, the sedimentary rocks of the terrane locally are thrust
onto the Onon terrane.

In Mongolia, terrane consists of: (1) Silurian(?) shallow marine
sedimentary rocks; (2) Early to Middle Devonian basalt, andesite, tuff,
chert, volcanoclastic sandstone; (3) Middle to Late Devonian sandstone,
siltstone with olistostrome, and red chert containing Famennian
conodonts; and (4) Early to Late Carboniferous interbedded sandstone,
siltstone, chert, and minor boulder conglomerate. Terrane is overlain by
Early Permian felsic volcanic rocks, Late Permian conglomerate,
sandstone and siltstone with abundant flora, and Middle to Late Triassic
and Jurassic sedimentary rocks. Postaccretionary granite rocks are the
Late Carboniferous to Early Permian Hangay pluton belt and Late Triassic
to Jurassic REE granite. The terrane is interpreted as a Devonian to
Carboniferous accrettionary wedge composed dominantly of turbidite.

**REFERENCES**: Zonenshain and others, 1990; Teraoka and others, 1996;
Kurimoto and others, 1997; Zorin, 1999, Parfenov and others, 1999b.

In the Transbaikalia, oldest part of the terrane consists of
Paleoproterozoic metamorphic formations (Uleleisky sequence) that
contains granitized biotite, biotite-muscovite, and biotite-amphibole
gneiss, quartz-biotite and biotite-muscovite schist, marble limestone
lenses, quartzite, and amphibolite. The lower part of the sequence
contains mainly gneiss, and the upper part contains mainly schist. These
rocks form xenoliths in the massifs of early Paleozoic granitoids that
mainly consist of anatectic granites of a wide compositional range with
smaller amounts of gabbro, gabbro-diorite, and diorite. The Late
Paleozic formations of the Transbaikalia region include sedimentary
rocks of the Devonian(?) Agutsinsky and Goryachinsky suites, Early
Carboniferous Ingodinsky formation, and Late Carboniferous Gutaisky
suite that contains brachypods and bryozoans. The Devonian and
Carboniferous units consist of terrigenous sequences of alternating
greywacke and polymictic sandstone, siltstone, and local conglomerate
and limestone. The Agutsinsky suite and Ingodinsky formation contain
mainly lenses of jasper, the mafic and intermediate volcanic rocks. The
close spatial association of terrigenous sedimentary rocks, mafic and
intermediate volcanic rocks, and jasperoid pf Devonian and Carboniferous
age are interpreted as a subduction melange. The sedimentary rocks are
intruded by calc-alkaline granitoids of the Late Carboniferous Daurian
complex that occurs in large batholith-like plutons.

The Permian and Early Triassic Selenga and Middle Jurassic through Early
Cretaceous Trans-Baikalian-Daxinganling sedimentary-volcanic plutonic
belt forms an overlap or suture complexe. The Early Jurassic sedimentary
rocks of the Dulankhor suite consist of variegated sedimentary breccias,
conglomerate, sandstone, and calcareous-clay shale with abundant plant
fragments and fresh-water bivalves are interpreted as continental
molasse. The terrane is interpreted as a Devonian to Carboniferous
accrettionary wedge composed dominantly of turbidite. The time of
accretion of the Khangay-Daurian terrane to the North-Asian Craton
occurred before the Permian as based on the overlapping Selenga belt
assemblage.

**REFERENCES**: Kotlyar and Popeko, 1974; Kozlov and Svadkovskaya, 1977;
Shergina and others, 1979; Zonenshain and others, 1990; Rutshtein and
Chaban, 1997; Parfenov and others, 1999; Zorin, 1999.

## HE Heilongjiang terrane (Accretionary wedge, type B) (Ordovician and Silurian) (Northeastern China)

## 

Consists chiefly of fault-bounded units of: (1) tectonic lenses or
olistoliths of marble and ultramafic rocks; (2) highly-deformed
mylonite, schist, gneiss, amphibolite, and glaucophane schist; and (3)
pillow basalt. Heilongjiang terrane generally metamorphosed to
glaucophane schist facies. Whole rock ^40^Ar/^39^Ar age of of
glaucophane schist is 455 Ma to 410 Ma. Terrane is interpreted as an
accretionary wedge which was thrust over the Jiamusi terrane during
accretion of Jiamusi terrane and Zhangguangcailing terrane. The
northeast-striking part of Heilongjiang terrane is displaced by
Dunha-Mishan Fault. Local blueschist facies metamorphism with occurrence
of glaucophane.

**REFERENCES**: Dong, 1990; Zhang Xingzhou, 1991; Cao Xi and others,
1992; Zhang and Sklyarov, 1992; Ye Huiwen and others, 1994; Tang Kedong,
1995; Sun Jiapeng and others, 2000.

## HG Hegenshan terrane (Accretionary wedge, type B) (Devonian through Permian) (Southeastern Mongolia, Northeastern China)

## 

In southeastern Mongolia, forms wedge shaped block, squeezed between
Nuhetdavaa and Hutag Uul terranes. Consists of variably metamorphosed
and sheared rocks that includes: (1) Undated quartz-feldspar schist and
gneiss; (2) Devonian calc-alkalic basalt, andesite, dacite, and
volcaniclastic rocks, and minor limestone with brachiopods, corals and
bryozoans; and (3) Early to Middle Carboniferous, shallow-marine,
sedimentary rocks and coeval andesite to rhyolite volcanic rocks. These
unites are unconformably overlain by Permian andesite, dacite,
tuffaceous sandstone, siltstone, and minor fusulinid-bearing limestone
that stitched together by Late Carboniferous and Permian granite, and
Triassic to Early Jurassic alkalic granite. Terrane interpreted as
displaced fragment of the Hegenshan ophiolite suture zone.

**REFERENCES**: Rhuzentsev and others, 1992; Badarch and Orolmaa, 1998;
Tomurtogoo and others, 2000.

In China, consists of ultramafic rocks extending 700 km along an
east-west strike and from 1 to 40 km wide. Ultramafic rocks are faulted
agains Devonian through Cretaceous strata, and are interpreted as an
ophiolite. Terrane consists of: (1) dunite, gabbro, olivine gabbro, and
tholeiite with intercalated radiolaria-bearing pillow basalt,
carbonatite, and tuff; (2) plagioclase-augite-peridotite with a K-Ar age
of 380 Ma and Devonian chert with tadiolaria; and (3) Cretaceous through
Permian marine carbonatite, terrigenous clastic rocks, and
volcaniclastic rocks that unconformably overlap the Devonian units. The
Hergenshan fault, along which the terrane occurs, is interpreted as one
of many important late-Paleozoic sutures between the Siberian plate and
the North China Cratopn. Terrane is interpreted as a fragment of an
accretionary wedge.

**REFERENCES**: Xie Tuolun, 1980; Liu Jiayi, 1983; Cao Congzhou, 1986;
Li Jinyi, 1987; Bureau of Geology and Mineral Resources of Inner
Mongolian Aut.Reg. (Inner Mongolian GMRB), 1991; Wang Quan, 1991.

## HI Hida terrane (Metamorphic) (Jurassic) (Central Japan)

## 

Consists of metamorphic rocks and Jurassic granites overlap by Jurassic
marine rocks and Jurassic to Early Cretaceous continental rocks. The
Hida metamorphic rocks exhibit high-temperature amphibolite facies
metamorphism that formed during Jurassic and Triassic igneous activity.
The Unazuki Schist, derived from Carboniferous to Permian sedimentary
rocks, formed in the Triassic during intrusion of igneous rocks. The
Funatsu Granite, with K-Ar ages clustered around 180 Ma, intrudes the
Hida metamorphic rocks and Unazuki Schist.

**REFERENCES**: Shibata and Nozawa, 1984; Adachi and others, 1992.

## HL Herlen terrane (Oceanic) (Late Neoproterozoic through Early Cambrian) (Eastern Mongolia)

## 

Occurs as a narrow fault-bounded lens up to 25 km wide and 200 km long
between the Argunsky and Idermeg terranes. Consists of: (1) Vendian to
Early Cambrian dismembered ophiolite, serpentinite melange,
gabbro-norite, gabbro, troctolite, and pyroxenite; and (2) Early
Cambrian tholeiitic basalt, andesite basalt, tuff, chert, and
volcaniclastic sandstone, siltstone, minor conglomerate, and limestone.
Post-accretion granitic rocks are Middle to Late Cambrian(?)
granodiorite and granite. Terrane is overlain by Middle to Late Triassic
and Jurassic nonmarine sedimentary rocks and intruded by Middle to Late
Carboniferous, and Late Triassic to Early Jurassic granite plutons.
Terrane is deformed into a series of tectonic sheets that are seperated
by north-verging thrust faults. Both the Paleozoic and Jurassic rocks
are folded and thrusted toward the north. Terrane is interpreted as
displaced fragment of dismembered ophiolite or suture zone.

**REFERENCES:** Tectonics, 1974; Palei and Juravleva; 1978, Agafonov and
Stupakov, 1983; Tomurtogoo, 1989, Byamba, 1996.

## HM Hamar-Davaa terrane (Metamorphic) (Paleoproterozoic through Early Cambrian) (Mongolia, Transbaikalia)

## 

In Mongolia, forms a northeast-east trending belt that extended for 400
km from northeast of Hovsgol lake to the southern side of the Baikal
Lake in Transbaikalia region. Consists of: (1) Paleoproterozoic
high-grade metamorphic rocks, including gneiss, schist, amphibolite, and
marble; and (2) Late Riphean to Early Cambrian schist, quartzite,
rhyolite, and marble. Metamorphic rocks of the Khamardavaa formation
(Transbaikalia) have a Pb-Pb isotopic age of 1120± 110 Ma. Terrane is
overlain by Silurian marine sedimentary rocks and intruded by Middle
Ordovician and Devonian granodiorite and granite. The tectonic
affinities and paleogeography of the Hamardavaa terrane are not clear.
The terrane may be craton fragment or a metamorphic terrane that
collided with Siberian continent in the Late Riphean, or fragment of a
metamorphosed, back-arc basin or continental margin arc. The terrane is
interpreted herein as a metamorphic terrane of uncetain affinity,
possibly a displaced fragment of a cratonal terrane.

**REFERENCES**: Belichenko and others, 1988, 1994, Dobretsov and others,
1989, Parfenov and others, 1995, 1996; Zorin and others, 1994;
Khomentovsky and Gibshir 1996; Tomurtogoo, 1997; Bulgatov, 1998.

In Transbaikalia region, terrane extends northeast from the Khubsugul
Lake in the south through the Khamar-Daban ridge where it strikes
sublatitudinally and further along Lake Baikal. Consists of the
Khamar-Daban and Olhon subterranes.

Khamar-Daban subterrane consists of metamorphic rocks of the Sludianka,
Khangarul and Khamar-Daban series, of debateable age from the Archean to
the Proterozoic. U-Pb zircon isotopic ages of 481±5 through 474±5 Ma are
interpreted as the age of granulite metamorphism. The Sludianka series
includes hornblende-pyroxene schist schist, gneiss derived from
graywacke, and marble and calc-granofels. The Khangarul series
unconformably overlies the Sludianka series and consists of diopside
schist, derived from andesite, and biotite gneiss, derived from
graywacke, with interbeds of marble and calc-granofels. The Khamar-Daban
series consists of the Bezymyansky carbonate-gneiss, Cornilovsky schist,
and Shubutuy carbonate-gneiss-schist. Terrane exhibits zonal
metamorphism, including kyanite-sillimanite and andalusite-sillimanite
granulite facies. The U-Pb zircon age of syn-metamorphic, two-pyroxene
plagiogranites is 481±5 Ma, and 474±5 Ma for post-metamorphic quartz
syenite. Undated large masses of biotite and amphibole-biotite
granitoids occur in the central parts of subterrane. Occurrence in areas
amphibolite facies of metamorphism, and occurrence of granite-pegmatites
and orthotectites within the granulite facies suggests granitoid
formation during Ordovician zonal metamorphism.

The Olkhon subterrane consists of sedimentary rocks of the Olkhon and
Anginsky series. The Olkhon series contains two-pyroxene and
diopside-hornblende plagioschist, amphibolite, and biotite-amphibole
schist derived from tholeiite metavolcanic rocks, small bodies of gabbro
and ultramafic rocks, and biotite-garnet, biotite plagiogneiss and
schist derived from greywacke, carbonate and calc-silicate sedimentary
rocks. The Olkhon series is characterized by intensive granitization
with formation of migmatite-granite domes. The Anginsky series contains
marble and siliceous rock, amphibolite, and calc-silicate rocks that are
metamorphosed to amphibolite and epidote-amphibolite facies. Amphibolite
is derived from andesite basalt. The Anginsky series is interpreted as
forming in a calc-alkaline island arc with final-stage eruption of
alkaline basalt. Metagabbro and ultramafic rockss are small bodies in
tectonic slabs. Locally, gabbroic rocks of the Ozersky complex form
large masses. One gabbro body has a Sm-Nd isochron age of 530±23 Ma, and
a U-Pb zircon metamorphic age of 485±5 Ma. Zonal metamorphism varies
from granulite to epidote-amphibole facies.

**REFERENCES**: Pavlovskiy, Eskin, 1964; Shafeev, 1970; Vasiliev and
others, 1981; Bibikova and others, 1990; Makrygina and others, 1993;
Fedorovsky, 1995, 1997; Kotov and others, 1997.

## HU Hug terrane (Accretionary wedge, type B) (Neoproterozoic) (Northern Mongolia, Eastern Sayan)

## 

In Mongolia, forms south-north trending narrow belt, between the
Sangelin and Sarkhoy terranes. Forms a structurally complex assemblage
of:1) Shishigt ophiolite composed of metaperidotite (with a thickness of
3.5 to 4.0 km), harzburgite, dunite, minor lherzolite, and
clinopyroxene-bearing harzburgite, wehrlite, clinopyroxenite, layered
gabbro, and diabase (800 m thick) with an uppermost part of
plagiogranite; (2) Middle Riphean low potassium tholeiitic metabasalt,
tuff, chert, metasandstone, phyllite, and minor dolomite (Hug series)
with a minimum structural thickness of 6,300 m. The metabasalt is
interpreted as forming in within plate settings or as an oceanic island
tholeiite. The Riphean rocks are metamorphosed to blueschist facies with
crossite, actinolite, winchite, and retrograded to
greenschist-blueschist facies. A Rb-Sr isochron age of 829± 23 Ma exists
for blueschist facies metamorphism, and 624±52 Ma and 640±20 Ma for
greenschist facies metamorphism. Terrane occurs in a number of thrust
slivers and sheets, and is overthrusted to the east along the Doodnuur
thrust that contains breccia and slivers of Vendian to Early Cambrian
limestone and dolomite. Postaccretion plutonicrocks are early Paleozoic
diorite and granodiorite with Rb-Sr isochron ages of 491± 25Ma, Devonian
alaskite granite, and nephelinite syenite. The Hug terrane is
interpreted as an accretionary wedge that formed during the collision of
the Sangelin block with the Sarkhoy island arc. Terrane is overlapped by
the Vendian-Cambrian Boksonsky series.

**REFERENCES:** Sklyarov and Dobretsov, 1987; Dobretsov and others,
1989; Dobretsov, Kirkdyashkin, 1993; Kuzmichev, Zhuravlev, 1996;
Sklyarov and others, 1996; Tomurtogoo, 1997; Enkhbat, 1999.

In southeastern Transbaikalia region, terrane extends in a
sublatitudinal direction for over 125 km and ranges up to 25 km wide. A
smaller volcanogenic part of the terrane contains of diabase, basalt,
and mafic tuff, and small ultramafic rock and gabbro bodies. The larger
part of terrane contains terrigenous-tuffaceous sedimentary rocks. The
terrane is metamorphosed to blueschist. The gabbroic sills exhibit a
Sm-Nd isochron age of 736±43. Before the Vendian, the terrane was
amalgamated with the Ilchir, Gargansky, Sarkhoy and Dibinsky terranes to
form part of the Tuva-Mongolian microcontinent. Terrane is overlapped by
the Vendian-Cambrian Boksinsky series.

**REFERENCES**: Sklyarov, Dobretsov, 1987; Geology and ore-bearing
capacity of Eastern Sayan, 1989; Kuzmichev, Zhuravlev, 1996.

## HV Hovd terrane (Continental-margin turbidite) (Neoproterozoic through Silurian) (Mongolia Altay)

## 

Occurs in the eastern foothills of the Mongolian Altay range and forms a
narrow northwest trending belt between the Tolbonuur and Tsagaanshiveet
strike-slip faults. Consists of a series of highly sheared and faulted
slivers of: (1) Vendian to Cambrian(?) basalt, andesite, gabbro, and
serpentinite melange, (2) Middle and Late Cambrian sandstone and
siltstone metamorphosed to greenschist and amphibolite facies, and minor
melange and olistostrome; (3) Early to Middle Ordovician sandstone,
graptolite shale, and argillite; (4) Middle to Late Ordovician
conglomerate, sandstone, siltstone, and limestone; and (5) Silurian
spilite, diabase, sandstone, siltstone, and graptolite shale that are
intruded by gabbro, diorite, granodiorite, and plagiogranite with K-Ar
ages of 456-440 Ma. Boundaries between tectonic blocks and slivers are
mainly strike-slip faults. Terrane is overlain by Devonian volcanic
plutonic rocks, and Early to Middle Carboniferous volcanic-sedimentary
rocks. Postaccretion granitic rocks are Devonian to Permian subalkaline
granite, and Jurassic leucogranite. Terrane is interpreted as early
Paleozoic continental margin turbidite basin that formed along a
transform margin.

**REFERENCES**: Dergunov and others, 1980; Rozman, 1986; Volochkovich
and Leontyev, 1990; Rhuzentsev and others, 1991; Berzin and others,
1994; Berzin, 1995; Byamba and Dejidmaa, 1999.

## HX Hutaguul-Xilinhot terrane (Metamorphic) (Paleoproterozoic and Neoproterozoic) (Mongolia, Northeastern China)

## 

In northeastern China, extends in an east-west direction and consists
mainly of Paleoproterozoic phyllite, slate, quartzite, quartz schist,
marble, and other low-grade greenschist facies rocks. Terrane is
intruded by Devonian and Triassic granite, the latter with K-Ar isotopic
age of 229 Ma, and is overlapped by the Jurassic and Cretaceous volcanic
rocks

**REFERENCES**: Dong Shenbao, 1983; Bureau of Geology and Mineral
Resources of Inner Mongolian Aut.Reg. (Inner Mongolian GMRB) 1991.

In southeast Mongolia, forms an east-west elongated block, north of
Sulinheer terrane and is composed of: (1) Paleoproterozoic gneiss,
schist, migmatite, marble, and quartzite; (2) Early to Middle Riphean
schist, metasandstone, phyllite, minor marble, and limestone; (3) Middle
to Late Riphean marble, quartzite, and limestone with stromatolites and
oncolites; and (4) Devonian basalt, andesite, dacite, tuff,
volcaniclastic sandstone, siltstone, phyllite, minor pillow basalt, and
limestone with corals and crinoids. Preaccretion plutonic rocks includes
Middle to Late Devonian granite and granodiorite. Terrane is
unconformably overlain by Permian volcanic rocks and marine turbidite,
and Early Cretaceous rocks. Terrane is intruded by Permian leucogranite,
syenite, and Early Triassic alkalic granite. Trrane is interpreted as a
displaced fragment of a cratonal terrane.

**REFERENCES**: Suetenko and Lkhasuren, 1973; Ruzhentsev and others,
1989, 1992; Badarch, 1990; Tang, 1990; Permian, 1991; Hsu and others,
1991; Byamba, 1996.

## IB Izu-Bonin terrane (Island arc) (Miocene through Quaternary) (Japan)

## 

Consists of basalt and andesite rocks ranging in age from Miocene to
Quaternary. Miocene submarine formation consists of altered basalt and
andesite, and minor clastic rocks. Many Quaternary volcanoes occur in
the terrane. Terrane exhibits crustal structure typical of oceanic
island arcs with about a 25-km-thick crust. The crustal structure is
interpreted as: (1) upper volcanic rocks and pyroclastic layer; (2)
intermediate tonalite layer; and (3) deeper mafic amphibolite layer.
Terrane is interpreted as accreting onto the Japanese islands as the
result of northward subduction of Philippine Sea Plate. Accretion of the
island arc crust formed a collisional zone at the northern margin of the
terrane. Tanzawa tonalite in the collision zone is interpreted as the
intermediate layer of the island arc.

**REFERENCES**: Aramaki and others, 1990.

## ID Idermeg terrane (Passive continental margin) (Proterozoic and Cambrian) (Eastern Mongolia)

## 

Bounded by Herlen fault to the north and Ondorshil fault to the south.
Terrane basement exposed in scattered small blocks (Idermeg, Bayan Terem
and Middle Gobi, Oortsog blocks). Terrane consists of: (1)
Paleoproterozoic gneiss, amphibolite, schist, and quartzite with K-Ar
isotopic ages of 1050, 1120, and 970 Ma; (2) Middle to Late Riphean
quartz-amphibole, quartz-biotite amphibole, and quartz-sericite-chlorite
schist, and phyllite, quartzite, marble, and limestone with
stromatolites and oncolites; and (3) unconformably overlying Early
Cambrian sandstone, siltstone, phyllite, quartzite, minor conglomerate,
and limestone with archeachyathids. Terrane is intruded by Middle to
Late Riphean, and Middle to Late Cambrian granite and granodiorite, and
is overlain by Devonian, Permian, Triassic, Jurassic sedimentary and
volcanic rocks, and is stitched together by Carboniferous, Permian, and
Mesozoic granite plutons. Terrane is interpreted as a fragment of
passive continental margin that was overlapped by Permian continental
margin arc, or as a fragment of a microcontinent.

**REFERENCES**: Amantov, 1966; Byamba and others 1990; Belichenko and
others, 1994; Byamba, 1996; Parfenov and others, 1999b; Zorin, 1999.

## IG Igarka terrane (Island arc) (Neoproterozoic) (Yenisey Region)

## 

Terrane occurs along the Yenisey River, extends submeridional direction
for100 km, and ranges up to 20-25 km wide. Consists of basalt, pillow
basalt, andesite and basalt porphyry, tuff, and spilite with
interlayered green and black shale, and quartz sandstone, and
tuff-breccia containing a great quantity of schist debris, and
metamorphosed limestone and dolomite. Intrusive complex include diabase
sills and dikes, quartz porphyry, and granodiorite. Terrane is
unconformity overlain by Late Riphean carbonate and
terrigenous-carbonate deposits that are unconformity overlain by
Vendian-Cambrian terrigenous-carbonate units. Nappes with volcanogenic
rocks are thrust eastward onto the Precambrian carbonate and
terrigenous-carbonate deposits towards the Siberian Platform.

**REFERENCES**: Postel'nikov, 1989; Nekrasov and Berendeev, 1991.

## IH Ih Bogd terrane (Oceanic) (Neoproterozoic and Early Cambrian) (Gobi Altay, Southwestern Mongolia)

## 

Occurs chiefly in two narrow, fault-bounded thrust sheets that range up
to one km wide and 6 to 15 km long, and in several other small lenses.
Consists of deformed and poorly studied fragments of serpentinite
melange and dismembered ophiolite, presumably Vendian to Early Cambrian
ages. The serpentinite melange contains numerous blocks of amphibolite,
pyroxenite, and metamorphic rocks. The ophiolite consists of
serpentinized harzburgite, minor dunite with rodingite veins, layered
gabbro with inclusions of pyroxenite and wehrlite, and dike swarms. The
dike complex consists of subparallel diabase and basalt dikes, and
screens of hornblende diorite. Terrane also contains Vendian to Early
Cambrian(?) spilite, keratophyre, basalt, andesite, tuff, sandstone,
phyllite, limestone with stromatolites and oncolites. Terrane intruded
by Early Permian leucogranite and unconformably overrlain by Late
Permian and Jurassic volcanic and sedimenary rocks. Terrane is
interpreted as displaced fragment of ophiolite that between Idermeg and
Gobi Altay terranes.

**REFERENCES:** Perfiliev and Kheraskov 1980; Byamba, 1996; Tomurtogoo
and others, 2000.

## IL Ilchir terrane (Oceanic)(Neoproterozoic through Ordovician) (Eastern Sayan, Mongolia)

## 

In Mongolia, occurs in small 25x30 km area, north of Huvsgol lake,
between Gargan terrane to the west and Hamardavaa terrane to the east.
The terrane comprises a Neoproterozoic dismembered ophiolite complex
containing dunite, harzburgite, gabbro, and Middle Cambrian to Early
Ordovician sandstone, siltstone, and tuff intruded by Late Ordovician
granite and granodiorite.

**REFERENCES**: Belichenko and others, 1988; Parfenov and others, 1995.

In the southeastern Eastern Sayan, terrane extends in a sublatitudinal
direction for over 200 km with ranges up to about 25 km wide. Consists
of: (1) a Riphean ophiolite composed of restite ultramafic rock, mafic
flows and pillow lava, siliceous-terrigenous sedimentary rocks, and
olistostrome (Ospinsky suite); and (2) Vendian to lower Cambrian island
arc volcanic rocks. The ophiolite exhibits a U-Pb zircon age of 1010 Ma.
After pre-Vendian amalgamation with Sarkhoy island arc terrane, Dibinsky
and Khugeinsky turbidite basin terranes, and Gargansky cratonal terrane,
these terranes were overlapped by Vendian-Cambrian sedimentary rocks
(Bokson series) that consist Middle Cambrian to Early Ordovician
sandstone, siltstone, and are intruded by Ordovician granite and
granodiorite.

**REFERENCES**: Dobretsov and others, 1985; Belichenko and others, 1988;
Parfenov and others, 1995; Khain and others, 1999.

## IM Imjingang terrane (Accretionary wedge, type B) (Devonian) (Korea)

## 

Consists of Devonian terrigenous rocks and volcanic rocks (Rimjin
Group). Terrigenous rocks are conglomerate, sandstone, and shale with
limestone layers. Mafic and siliceous volcanic rocks occur in the upper
part of the section. Fauna and flora remains reveal rather irregular
stratification, with some layers with Middle Devonian flora
overthrusting layers Late Devonian brachiopods.

**REFERENCES**: Geology of Korea, 1993.

## IS Isakov terrane (Island arc) (Neoproterozoic) (Yenisey Ridge)

## 

Terrane extends in a submeridional direction fornearly 300 km long,
ranges up to 50 km wide, and is thrusted onto the West Angara passive
continental margin terrane situated to the east. Consists of Late
Riphean volcanic-sedimentary units and ophiolites. Central part of the
terrane consists of oceanic rock complex including fragments of
ophiolite (metaperidotite, metagabbroic rocks, and tholeiite basalt),
and phyllite, and carbonate-bearing quartz-mica schist. Locally
occurring are parallel diabase and diabase-porphyry dikes and sills
intruding metabasalt. To east and west of paleooceanic units are
calc-alkaline metarhyolite and metaandesite-basalt flows, metamorphosed
tuff, tuffaceous sandstone, sandstone, phyllite, shale, and limestone.
The island arc Porozhnensk plagiogranite has a U-Pb zircon isotoic age
of 697±3.6 Ma (V. Vernikovsky and others, this report); this age is
interpreted as the upper age boundary of the formation of island arc and
ophiolite. Metamorphic minerals from metamafic rocks and metapelite have
Rb-Sr and K-Ar isotopic ages of 600-620 Ma studies and are interpreted
as time of terrane obduction onto the passive craton margin. Complexes
in terrane are thrust bounded. Schist adjacent to faults are corrugately
recrumpled, altered, and silicified with faulted carbonate rocks. Zones
of serpentine melange occur within ultramafic rocks. Metamorphism in the
southern and eastern parts of terrane ranges up to epidote-amphibolite
facies with garnet in schist in metabasalt. To the north and west, away
from terrane boundaries, metamorphism grade ranges to lower greenschist
facies. Terrane is unconformity overlapped by Late Riphean and Early
Cambrian terrigenous-sedimentary deposits of the Vorogovka-Chapa
sedimentary assemblage.

**REFERENCES**: Mironov, Nozhkin, 1978; Postel'nikov, 1980; Kuzmichev,
1987; Vernikovsky and others, 1993, 1994.

## JI Jiamusi terrane (Metamorphic) (Neoproterozoic and older and Early Cambrian) (Northeastern China)

Consists chiefly of: (1) sillimanite schist, quartz schist, felsic
gneiss, graphite schist, and marble (Mashan Group) with thickness of
over 9,000 m; and (2) migmatite, gneiss, quartz schist, graphite schist,
banded iron formation, and marble (Xindong Group) with a thickness of
over 7300 m; and Neoproterozoic-Early Cambrian carbonate and
terrigeneous deposits. The oldest overlap assemblages are: (1) Early
Devonian sandstone and slate (Xinzhong Formation) that unconformably
overlay the Precambrian basement; (2) Middle and Late Devonian
sandstone, slate, limestone, and dacite tuff (Qiligeshan Formation,
Shangheitai Formation and Xiaheitai Formation); (3) Early Carboniferous
sandstone and tuff; (4) Late Carboniferous tuff, sandstone, and slate
and conglomerate (Tatouhe Formation, Zenzishan Formation, Guangqing
Formation); (5) Early Permian siltstone and tuff (Erlongshan Formation),
(6) Late Permian conglomerate, sandstone and slate (Chenshan Formation);
(7) Early Cretaceou sandstone and conglomerate; and (8) Mesozoic and
Cenozoic sedimentary rocks. The Jiamusi terrane underwent several times
of regional metamorphism, and the highest metamorphism reach granulite
facies. The oldest metamorphic age is 1300 Ma and the youngest
metamorphic age is 500 Ma.

**REFERENCES**: Zhang Qinglong and others, 1989; Shao Jian and others,
1991;Cao Xi and others, 1992; Tang Kedong and others, 1995; Jiang
Jisheng, 1996; Bureau of Geology and Mineral Resources of Heilongjiang
(1993); Krasnyi and others, 1996, Wilde and others, 1997, 1999; Sun
Jiapeng and others, 2000.

## JT Japan trench terrane (Accretionary wedge, type A) (late Tertiary and Quaternary) (Western Pacific Ocean)

Consists chiefly of trench slope and trench fill deposits of Miocene
through Quaternary sedimentary rocks in Japan and Izu-Bonin trenches.
Contains a gravitational slide zone on inner trench slope. The trench
interpreted as a tectonic errosion type. Coarser-grained sedimentary
rocks are more dominant in the Quaternary section than in late Miocene
and Pliocene section. The Quaternary sedimentary section consists of
sediments formed in a forearc basin, in a slope basin, and on a trench
floor. The latter are coarser-grained and accumulated more rapidly than
the clay-rich sedimentary rocks on the trench slope. The lower slope
contains a relatively large number of channels and a greater amount of
slumped material than elsewhere. Channels commonly corss the forearc
basin and trench slope, and provide transport paths for coarse-grained
sediment to various parts of the margin.

**REFERENCES:** Von Huene and Arther, 1982, Wakita and others, 1992.

## KA Kan terrane (Cratonal) (Paleoproterozoic) (Eastern Sayan)

## 

Contains komatiite-basalt, tholeiite-basalt, leucobasalt,
andesitobasalt, andesite-dacite-rhyolite, graywacke, and sparse
carbonate rocks. Metamorphosed to amphibolite facies. Amphibolite and
amphibole-gneiss with lenses and horizons of metaultramafic rocks
predominate. Greenschist diaphthorites occur along bounding faults. Core
of terrane contains granite-gneiss domes and linear, tectonically
imbricated zones. U-Pb zircon ages for metamorphic rocks range from 1.7
to 2.3 Ga. K-Ar mica ages range from 530-560 Ma, and Rb-Sr biotite
isochron age is 560 Ma. The age range indicates several superimposed
thermal processes. Terrane contains plutons of various ages. The oldest
are mafic massifs, now metagabbro, metadiorite, and epidote-amphibolite
schist with K-Ar amphibole isotopic age of 1175 Ma. Younger
tonalite-tondjenite in the domes has a U-Pb zircon isotopic age of 1900
Ma and a Pb-Pb age of 1860 Ma, and a U-Pb orthite age of 1800 Ma.
Similar K-Ar mica ages occur. Terrane intruded by Early Devonian syenite
and granosyenite plutons, and is locally overlapped by Devonian
volcanic-sedimentary units of the South Siberian rift-related
volcanic-plutonic belt. Terrane is interpreted as a fragment of the
Early Precambrian basement of the North Asian Craton that was displaced
along the Main Fault in Eastern Sayan towards the Kuvai terrane.

**REFERENCES**: Polkanov and Obruchev, 1964; Volobuev and others, 1980;
Nozhkin and others, 1989, 1996; Rumyantsev and others, 1998; Tsypukov
and others, 1993; Rozen and others, 1994.

## KBG Kabarga terrane (Accretionary wedge, type A) (Neoproterozoic and early Paleozoic) (Southern Russian Far East) 

## 

Occurs in an east-west-trending band from 10 to 25 km wide north of Lake
Khanka between the Matveevka and Nakhimovka terranes. Consists of
following units. (1) Micaceous schist interlayered with quartzite
(Spassk Formation) occuring at the base and overlying, less
metamorphosed graphite-muscovite schist interlayered with amphibolite
and limestone (Mitrophanovsk Formation), with an overlying sequence of
phyllite and sandstone resting (Kabarga Formation and jaspilite
sequence). Total thickness of deposits about 2,700 to 3,000 m. (2)
Overlying carbonate rocks (Smolinsk and Rudonosny Formations). The
Smolninsk Formation consists of dolomite and limestone interbedded with
chert and shale. The overlying Rudonosny Formation consists of: (1) a
lower layer (80 m thick) of shale and graphite shale; (2) an
intermediate ore-bearing layer (10-100 m thick) of jaspilite,
ferromanganese, manganese, phosphorite siliceous ore and gangue
quartzite; and (3) an upper layer (10-300 m thick) of shale interbedded
with dolomite and limestone. The carbonate rocks are limestone and
dolomite, intercalated with shale, and is about 700 m thick. The age of
the Rudonosny Formation is assumed to be Early Cambrian, by analogy with
similar fossiliferous deposits in the Maly Khingan Ridge area. Terrane
also contains locally outcrops of serpentinite melange, and is deformed
into a system of closely spaced folds of east-west, less common
northwest and northeast trends.

**REFERENCES**: Khanchuk and others, 1996.

## KBN Kalba-Narim terrane (Accretionary Wedge, type A) (Ordovician through Early Carboniferous) (Kalba-Narim area)

## 

Occurs between the Devonian-Carboniferous Rudny Altai and Zharma-Saur
island-arc terranes. Consists of three units (from northeast to
southwest), Irtysh-Kurchum, Kalba-Narim and Chara. Irtysh-Kurchum unit
chiefly composed of Early-Middle Devonian ane lesser Silurian
sedimentary rocks, locally with olistostromes and lenses of
serpentinitic melange. The Kalba-Narim unit consists of a monotonous
Late Devonian and Early Tournaisian black shale turbidite sequence. The
Chara unit consists of Early Carboniferous marine terrigenous, mainly
sandstone and sandy siltstone, flysch sequence, and associated
olistostrome and melange of the Chara ophiolitic belt or suture. The
olistostromes and melange contain rocks of variable composition. The
ophiolites consist of basalt and deep-water siliceous rocks, including
units formed in seamounts, island-arcs, and reefs that contain abundant
radiolaria, conodonts, graptolites, brachipods, and foraminifera of
Ordovician(?) through Early Carboniferous age. Locally, the melange
contains blocks of eclogite, garnet amphibolite, glaucophane, and
winchite schist. K-Ar isotopic ages of high-pressure rocks range from
360-370 to 540-570 Ma. The Chara melange-olistostrome unit is
structurally complicated and contains fragments of an accretionary wedge
and island arc that may have fromed from extensive strike-slip
displacement along a convergent continental margin. This unit and marine
flysch-like sequences are overlapped by Middle-Late Carboniferous
continental terrigenous deposits with lesser coal and volcanic rocks
that are interpreted as a transition collisional. The intrusion of giant
Late Permian-Early Triassic granitic plutons of the Kalba belt are
interpreted as forming in the final stage of oblique collision during
late Paleozoic and early Mesozoic strike-slip displacement along major
faults such as the Irtysh strike-slip fault. Close to the fault, the
degree of metamorphism ranges from lower greenschist to amphibolite
facies the occurred during imbricated thrust and strike-slip
deformation.

**REFERENCES**: Ermolov and others, 1981; Rotarash and others, 1982;
Berlin and others, 1994; Iwata and others, 1994.

## KE Kema terrane (Island arc) (late Early Cretaceous) (Southern Russian Far East)

## 

Occurs in the Sikote-Alin region and chiefly consists of distal
turbidite deposits, andesite and basalt flows, breccia, tuff, and
interbedded shallow-marine volcaniclastic rocks with Aptian to Albian
pelecypods. The volcanic rocks are mainly tholeiitic and calc-alkalic.
Terrane is overlain by late Albian and younger igneous rocks of the East
Sikhote-Alin volcanic-plutonic belt.

**REFERENCES:** Simanenko, 1986.

## KH Khapchan terrane (Granulite-paragneiss) (Paleoproterozoic) (Yakutia)

## 

Occurs in eastern Anabar shield and is bounded on the west by the
Billyakh strike-slip and reverse-fault melange zone. Consists mainly of
supracrustal rocks (Khapchan Group) including marble, calciphyres,
calc-silicate rocks, garnet paragneiss with up to 40% carbonate rocks,
and lesser enderbite and schist. Enderbites are similar to analogous
rocks of the Daldyn terrane that are interpreted as derived subalkali
and alkali basalt and andesite-basalt. Geochemical studies of the
Khapchan Group paragneiss suggest derivation of garnet gneiss from
graywacke, marble from limestone and dolomite, and calc-silicate rocks
from marl formed in a shallow-water shelf environment. Peak metamorphism
is middle granulite facies. Nd isotopic studies and Sm/Nd isotopic
ratios yield a model age of 2.4 Ga for the Khapchan Group. A U/Pb zircon
age of peak granulite metamorphism of is 2.0 Ga. The central and
southern parts of the terrane are deformed into tight linear folds,
whereas the northern part is deformed into several domes.

**REFERENCES**: Vishnevskiy, 1978; Lutz and Oxman, 1990; Rosen and
others., 1994.

## KHM Khamsara terrane (Island arc) (Cambrian) (Northeastern Tuva)

## 

Occurs in relatively small outcrops of Cambrian rocks between large
batholiths of Late Cambrian-Early Ordovician granitoids. Consists of two
blocks: (1) Early Cambrian rocks in an eastern block and in the eastern
part of the western block; and (2) farther west, Middle-Late Cambrian
and younger rocks. Blocks are separated by a northwest-striking zone of
metasandstone, metasiltstone, and metashale that may form a basement of
the Cambrian section or slope deposits related to volcanic arcs and
back-arc basins. Terrane consists of two units. (1) Khamsara suite with
a miniumum 2-2.5 km thickness that is chiefly composed of
andesite-basalt, andesite, and less siliceous volcanic rocks. The upper
part consists of tuff, tuff-breccia, tuffaceous conglomerate, tuffaceous
sandstone, siltstone, and limestone with Early Cambrian achaeocyata. (2)
The Irgitkhem suite that is composed of boulder-pebble conglomerate,
tuffaceous conglomerate, and andesite tuff and occurs only in the
western extremity of the terrane. The clastic material is dominated by
clasts of underlying volcanic rocks, and well-rounded granitic boulders
and pebbles. Rounded clasts and poorly-rounded/angular blocks and lenses
of limestone with Middle Cambrian trilobites are occur at various
horizons. The limestone is interpreted as syngenetic with the Irgitkhem
suite and formed in separated reers, or was redeposited to form
olistostrome-like horizons. The Irgitkhem suite is interpreted as
forming in the coastal part of a fore-arc trough during rapidly
attenuating island-arc volcanism, intensive tectonism, and strike-slip
movement along boundary of lithospheric plates.

**REFERENCES**: Chuchko and others, 1969; Bukharov, Zaikov, 1979;
Berzin, 1979, 1995; Berzin and Dobretsov, 1994; Berzin and Kungurtsev,
1996.

## KI Kanim terrane (Island arc) (Late Neoproterozoic and Early Cambrian) (Central Kuznetsk Alatau)

## 

The Kanim terrane forms an imbricate unit between the fragments of
back-arc structures and consists of four units. (1) Vendian and Early
Cambrian(?) sedimentary-volcanogenic rocks (Kanym and Tajozhny suites),
which is separated from the older deposits by faults. The main
lithologies are 4hyolite-dacite and andesite-dacite lava and tuff with
lesser mafic and andesite volcanic rock, black shale, and carbonate
rocks. (2) An Early Cambrian sedimentary assemblage of sandstone,
siltstone, shale, siliceous shale, and chert, layered
archaeocyata-bearing limestone, and sparse interlayers of mafic volcanic
rocks (Ustkundat suite). (3) An Aldanian-Early Lenian carbonate unit
composed mainly of massive limestone (Usin suite) with a rich fauna
including archaeocyata, trilobites, brachiopods, and other fossils. And
(4) a local, fault-bounded volcanic-sedimentary assemblage (Bogoyul
suite) that contains: (1) a lower part of mafic volcanic rocks with thin
interbeds of siliceous shale and shales; (2) a middle part composed of
shale, siliceous and mafic volcanic rock, volcaniclastic rocks, and
massive and layered limestone; and (3) an upper part composed of fine-
to coarse-grained clastic rocks with tuff lenses and Early Cambrian
limestone blocks with archaeocyata and trilobite. Terrane is interpreted
as a small fragment of a magmatic back-arc. Terrane is intruded by early
Paleozoic collisional granitoids, and is unconformity overlapped by
Early Devonian the sedimentary-volcanogenic complex of the South
Siberian rift-related volcanic-plutonic belt.

**REFERENCES:** Ekhanin, 1961; Gintsinger and others, 1969; Resolutions,
1979; Alabin, 1983; Grigor\'yev, 1988.

## KK Kizir-Kazir terrane (Island arc) (Cambrian) (Southwestern Eastern Sayan)

## 

The Kizir-Kazir terrane consists of thre major units that occur in
various tectonic lenses and sheets. The stratigraphic succession of
individual sequences, ages, and interrelationships are not clear. Three
units occur. (1) An Early Cambrian volcanic-terrigenous-carbonate
assemblage with unknown basement. In the most of the terrane the
assemblage is consists of reefoid limestone with trilobites,
archaeocyata, and brachiopodes (Atdabanian, Botomian and Toyonian
suites). In other areas, the assemblage consists of island-arc
tholeiitic volcanic rocks, related limestone, shale and siliceous shale,
and volcaniclastic deposits mainly in the eastern part of the terrane.
(2) A Middle Cambriam (Amgaian) assemblage of volcanic-sedimentary
deposits (Moiseev suite) containing trilobites and brachipods that
conformly overlaps the Early Cambrian carbonate sequences. This
assemblage consists of the following two suites. (a) A
terrigenous-volcanogenic suite occurs in the northeastern terrane and is
dominated by volcaniclastic rocks of variable grain size with
subordinate horizons of volcanic rocks and lenses/interbeds of siliceous
shale, limestone and carbonate-terrigenous rocks. And (b) a
carbonate-volcanic-terrigenous occurs mainly in the western part of the
terrane and is dominated by layered and massive limestone and calcareous
rocks with subordinate andesite and siliceous volcanic rock and tuff.
(3) A basalt-andesite calc-alkaline assemblage that unconformably
overlaps Early and Middle Cambrian rocks and is mainly composed of
pyroclastic material with subordinate sedimentary rocks (Kizir suite)
with an interpreted age of Middle Cambrian (Mayaian) through Late
Cambrian. Terrane is intruded by early Paleozoic collisional granitoids,
and Early Devonian(?) rift granitoids. Terrane is unconformity overlain
by Early Devonian rift-related sedimentary-volcanogenic complex and
Middle Devonian-Carboniferous continental molasse.

**REFERENCES**: Musatov and Nemirovskaya, 1961; Mezhelovsky, 1962;
Amgaian and others, 1971; Resolutions, 1979; Berzin and Kungurtsev,
1996.

## KLM Kiselyovka-Manoma terrane (Accretionary wedge, type B) (Jurassic and Early Cretaceous) (Southern Russian Far East)

## 

Occurs in a narrow band along the southern side of the Amur River
terrane, north of the Amur fault. Stratigraphy and structure are poorly
known. Distinguished from the adjacent Badzhal, Amur River, and Samarka
terranes by occurrence of Jurassic and Early Cretaceous ribbon chert and
siliceous shale, and Cretaceous flysch, Jurassic basalt and Early
Jurassic limestone. Terrane also contains chert and mafic volcanic rocks
in tectonic sheets and olistoliths in an Early Cretaceous olistostrome.
Terrane is interpreted as tectonically linked to the Khingan-Okhotsk
active continental margin.

**REFERENCES**: Filippov, 1988, Kuzmin, Kaidalov, 1990; Shevlyov, 1990,
Natal\'in, 1991.

## KM Kamensky terrane (Continental margin arc) (Early and Middle Triassic) (Transbaikalia)

## 

Occurs in the eastern part of Transbaikalia area, terrane extends in a
sublatitudinal direction for over 100 km and ranges up to 15 km wide.
Consists of volcanic-sedimentary rocks (Kamensky suite) and intrusive
rocks (Bereinsky complex) of island arc origin. The volcanic-sedimentary
rocks of the Kamensky suite consist of volcano-mictic conglomerate,
congloerate breccia, breccias, tuffaceous sandstone, and tuffaceous
siltstone. Coarse-grained lithologies predominate, and locally volcanic
rocks comprise up to 50% of the section. Volcanic rocks consist of
moderately- and high-aluminous basalt, andesite-basalt, andesite,
dacite, and rhyolite, and contain greenstone, propylitic, and albite
alteration. Volcanic rocks overlie Late Triassic sedimentary rocks
(Mogotuy Formation). The Bereinsky complex contains two intrusive
phases, an older phase of gabbros and diorite, and a younger phase of
mainly granite. The intrusive rocks constitute a
gabbro-diorite-trondjemite-plagiogranite association. Aluminiferous
gabbro comprises up to 50% of the complex and is associated with lenses
of amphibole-bearing peridotite (Rutshtein, 1973). Along the
Mongol-Okhotsk fault the intrusive rocks exhibit intense dynamic
greenschist facies metamorphism that is associated with Middle and Late
Jurassic strike-slip faulting K-Ar isotopic ages of 169-159 Ma (Dril and
Kuzmin, 1998). Overlap and stitching complexes formations are the Middle
Jurassic Trans-Baikalian-Daxinganling sedimentary-volcanic plutonic
(Karbachinsky continental-sedimentary suite), and Late Jurassic
granitoids (Kukulbey complex). These relations indicate a Pre-Middle
Jurassic accretion to the North Asian Craton.

**REFERENCES**: Dolganev, 1963; Kuzmin, 1985; Okuneva, Konditerov, 1964;
Rutshtein, 1973, 1997; Rutshtein and Chaban, 1997; Dril and Kuzmin,
1998.

## KN Kular-Nera terrane (Continental margin turbidite) (Permian through Early Jurassic) (Yakutia)

## 

Forms a broad, northwest-trending belt and consists chiefly of: (1) a
thick assemblage of Permian, Triassic, and Early Jurassic hemipelagic
and pelagic mudstone, siltstone, and minor sandstone; and (2) Permian
(Selennyakh Range) and Early Jurassic (Nera River) radiolarian chert and
tuff. Terrane is interpreted as a deep-sea-fan complex that contains
interbedded continental rise and marginal sea pelagic deposits that
formed between the passive margin of the Siberian continent (North Asian
Craton Margin) and terranes to the east. Terrane is weakly to highly
metamorphosed and deformed, and exhibits lower greenschist and locally
epidote-amphibolite facies. Terrane is locally deformed into gently
inclined appressed and superposed folds and is overlapped by the Middle
Jurassic to Early Cretaceous Indigirka-Oloy
sedimentary-volcanic-plutonic assemblage. Terrane is separated from the
Verkhoyansk foldbelt to the west by the Adycha-Taryn fault.

**REFERENCES**: Dagis and others, 1979; Parfenov and Trushchelev, 1983;
Parfenov and others, 1988, 1989; Bychkov and Kiseleva, 1990.

## KO Khor terrane (Island arc) (Early Paleozoic?) (Southern Russian Far East)

## 

Occurs in a narrow, fault-bounded wedge along the Cretaceous
sinistral-slip Central Sikhote-Alin fault. Terrane is surrounded by the
Samarka terrane and consists of gneiss, quartzite, and pelitic schist
that are metamorphosed to amphibolite and greenschist facies. Also in
the terrane are plagiogranite and leucogranite. The gneiss has a Rb-Sr
isotopic age of 227 Ma. The Khor and companion Anui terranes are
interpreted as parts of a single microcontinent that collided with the
eastern margin of Asia at the beginning of the Cretaceous. The Khor
terrane may correlate with the Sergeevka terrane.

**REFERENCES**: Zmievsky, 1980; Martynyuk, Mikhalev, and Popeko, 1986.

## KOZ Kozhukhov terrane (Island arc) (Late Neoproterozoic and Cambrian) (Northern Kuznetsk Alatau)

## 

Occurs in a small wedge-like block adjacent to the large Kuznetsk-Alatau
strike-slip fault. Three units are recognized. (1) Vendian(?)-Early(?)
Cambrian Contrasting volcanic rocks and tuff, clastic rocks, limestone,
chert, and siliceous shale (Kozhukhov and Chumai suites) with unclear
relations to older deposits are unclear. (2) Early Cambrian
conglomerate, gravelstone, sandstone, mafic tuff, and limestone with
archaeocyata (Karacharov suite). This sequence overlie the older
deposits with conformity, the others -- with unconformity and
interruption. Middle Cambrian (Amgaian) andesite and andesite-basalt
porphyry and tuff intercalated with volcaniclastic rocks,
sand-siltstone, sandy-shale, and limestone. The age is inferred from
correlation with the Berikul suite of the eastern Kuznetsk Alatau.
Terrane is overlapped by Early-Middle Ordovician marine molasse (Taimen,
Vasiliev and Bukhtai suites), Devonian sedimentary-volcanogenic units of
the South Siberian volcanic-plutonic belt, and Jurassic-Cretaceous
deposits of the West Siberian basin. Terrane is intruded by Early
Cambrian island-arc granitoids (Lavernov complex), Cambrian-Ordovician
collisional granite (Martaiga complex), and Middle-Late(?) granite and
granosyenite (Chebula complex) that may have formed in an active
continental margin.

**REFERENCES**: Resolutions, 1979; Alabin, 1983; Grigor\'yev, 1988.

## Kolyma-Omolon superterrane (Yakutia)

## 

Consists of a large number of cratonal, passive continental margin,
island arc, accretionary-wedge, and minor oceanic crust, and ophiolite
terranes. The superterrane is overlain by mainly Middle Jurassic to
Early Cretaceous Indigirka-Oloy sedimentary-volcanic-plutonic assemblage
that is interpreted as a pre-accretion marginal island arc assemblage.
The superterrane was accreted to the North Asian craton and the North
Asian Craton Margin during the Late Jurassic and Early Cretaceous. The
suture (Adycha-Taryn thrust fault) between the Kolyma-Omolon
superterrane and North Asian Craton Margin is intruded by the Late
Jurassic and Early Cretaceous Verkhoyansk collisional granite belt. The
eastern margin of the superterrane is locally extensively overlapped by
the Cretaceous and Paleocene Okhotsk-Chukotka volcanic-plutonic belt.

## KMN Munilkan terrane (Oceanic) (early Paleozoic) (Yakutia)

> Consists chiefly of the early Paleozoic(?) Kalgyn ophiolite that
> consists of serpentinized harzburgite, dunite, cumulate gabbro,
> amphibolite, and metabasalt with an Ar-Ar actinolite isotopic age of
> 415 Ma for metamorphism of the amphibolite. Terrane consists of
> several tectonic sheets that structurally overlie the early to middle
> Paleozoic carbonate deposits of the Omulevka terrane.
>
> **REFERENCES**: Shishkin, 1980; Dolgov and others, 1983; Arkhipov,
> 1984; Oxman, 1989; Parfenov and others, 1989; Layer and others, 1993.

## KOV Omulevka terrane (Passive continental margin) (late Neoproterozoic through Triassic) (Yakutia)

> Consists chiefly from base to top of five units: (1) Late
> Precambrian(?) marble, schist, and metavolcanic rocks; (2) an
> unconformably overlying thick unit (up to 1700 m thick) of boulder
> conglomerate with pebbles of native and exotic rocks, and Middle and
> Late fossiliferous Cambrian marble, schist, metarhyolite, and
> quartzite; (3) a thick sequence of Ordovician through Early
> Carboniferous fossiliferous carbonate rocks including limestone,
> dolomite, and marl, and sparse sandstone, siltstone, and mudstone; (4)
> Carboniferous and Permian fossiliferous tuff, chert, shale, limestone,
> siltstone, and sandstone; and (5) Triassic fossiliferous siltstone,
> mudstone, marl, and shaley limestone. Along the southeast border of
> the terrane is a unit of Givetian calcareous sandstone that contains
> marine trachybasalt flows. The deep-water siltstone, argillite, and
> chert that prevail in Famennian-Early Triassic section are
> interlayered with subordinate andesite and basalt tuff, and limestone.
> Except for the Late Permian, the late Paleozoic units contain numerous
> diabase sills that were cofolded with the host rocks. For
> paleomagnetic determinations, high-quality paleomagnetic directions
> from sedimentary rocks exist for two localities, one of Late Jurassic
> age, and the other of Middle Jurassic age. These determinations
> indicate a southward displacement with respect to the Siberian
> platform of 20^o^[+]{.underline}10^o^ for the older locality, and
> about 15^o^[+]{.underline}40^o^ for the younger locality. The Omulevka
> terrane is overlain by Jurassic volcanic rocks and intruded by coeval
> Jurassic granitic rocks of the Uyandina-Yasachnaya volcanic-plutonic
> belt (part of the Indigirka-Oloy sedimentary-volcanic-plutonic
> assemblage).
>
> **REFERENCES**: Merzlyakov, 1971; Bulgakova, 1986; Natapov and
> Surmilova, 1986; Parfenov, 1991; Neustroev and others, 1993.

## KPD Polousnyi-Debin terrane (Accretionary wedge, type A) (Jurassic) (Yakutia)

## 

> Includes units in the the Polousnyy and In'yali-Debin synclinoria
> located along the northwestern and southeastern margins of the
> Kolyma-Omolon superterrane, respectively.
>
> The Polousnyy synclinorium extends sublatitudinally for 500 km and
> ranges from 50-100 km wide. It is separated by thrusts from the
> Nagondzha and Omulevka terranes that occur to the south. To the west,
> the synclinorium borders on the Kular-Nera terrane along the thrust
> faults and, to the north, the synclinorium is overlain by Late
> Cenozoic rocks of the Primorsk lowland. The Polousnyy synclinorium
> consists of Jurassic turbidite deposits that range up to 5000 m thick.
> The lower part consists of interlayered shale and sandstone with
> endolistostrome horizons. The middle part consists of siltstone and
> sandstone. The Late Jurassic rocks in the northern part of the
> synclinorium are shale rich with rare sheets of andesite, andesite
> basalt, and basalt. Within the Primorsk lowland large positive gravity
> and magnetic anomalies exist and are interpreted as covered
> ophiolites. The Polousnyy synclinorium exhibits a fold-and-thrust
> structure, with related recumbent and inclined folds, and tectonic
> melange is widely, with greenschist facies metamorphism.
>
> The In'yali-Debin synclinorium extends in a narrow (70-100 km) arc for
> 800 km along the southwestern margin of the Kolyma-Omolon
> superterrane. The southwestern boundary of the In'yali-Debin
> synclinorium is the Charky-Indigirka thrust and other faults. The
> In'yali-Debin synclinorium consists of turbidite deposits up to 4,000
> m thick. The Middle Jurassic rocks consist of interlayered siltstone,
> mudstone, and sandstone with endolistostrome horizons. The Late
> Jurassic rocks consists of siltstone, clay shale, and polymictic and
> calcareous sandstone, with horizons of tuffaceous siltstone and
> sandstone and intraformational conglomerate. In the southern part of
> the In'yali-Debin synclinorium a tectonic sheet of ultramafic and
> mafic rocks occurs within the Jurassic sedimentary rocks. These rocks
> were previously described as the Debin ophiolite fragment. The base of
> the sheet consists of peridotite serpentinite, olivine, and
> hypersthene gabbro-norite, and anorthosite, whereas the upper part
> consists of banded two-pyroxene gabbro and gabbro-diorite.
> Petrochemistry of the gabbros indicates their formation from
> tholeiitic magma at various depths. The rocks of the In'yali-Debin
> synclinorium are deformed into compressed folds, including isoclines
> that are associated with high-angle, southwest-verging thrusts. The
> thrusts and folds are intruded by granitoid plutons that have
> 40Ar-39Ar isotopic ages of 139-143 Ma.
>
> **REFERENCES**: Chekhov, 1976; Gusev, 1979; Spector and others, 1981;
> Arkhipov, 1984; Oxman and others, 1995; Layer and others, in press.

## KNG Nagondzha terrane (Continental margin) (Carboniferous through Late Triassic) (Yakutia)

> Extends in a narrow band for 450 km and up to 100 kim wide to the
> north and west of the Ulakhan-Tas, Selennyakh, and Tas-Khayakhtakh
> blocks of the Omulevka terrane. Consists of repeatedly deformed, late
> Paleozoic and early Mesozoic rocks in packets of tectonic sheets and
> lenses of variable thickness. The oldest Carboniferous-Permian rocks
> form a series of small tectonic lenses and sheets along the eastern
> boundary of the terrane and consist of hemipelagic
> volcanic-terrigenous-siliceous and carbonate-terrigenous rocks with
> fragments of chert and pillow basalt. Ladinian and early Late Triassic
> sedimentary rocks contain a relatively homogeneous argillaceous
> composition and thin parallel bedding, with thin and pinching beds of
> calcareous sandstone and floating pebble sandstone that grade into
> rhythmically interlayered Late Triassic-Early Jurassic units of
> cross-bedded siltstone, shale, and calcareous sandstone. The section
> is topped with Bathonian-Callovian sedimentary rocks, including
> rhythmically interlayered calcareous sandstone, siltstone, and
> mudstone with olistostrom fragments of which grade along strike into
> conglomerate. A fold-and-thrust structure formed in at least three
> stages of deformation. The amount of horizontal shortening of
> stratigraphic section caused by thrusting is estimated at 35-40%, as
> based on balanced sections. Dextral and sinistral strike-slip faults
> are prevalent in the northeast and southwest parts of the terrane,
> respectively. The largest Setakchan thrust extends for 100 km as a
> band of melange and broken rocks. The Triassic rocks of the
> tectonically overlap Jurassic sedimentary rocks of the Polousnyy
> anticlinorium along the Setakchan thrust. The amount of horizontal
> displacement on the fault is estimated at a few tens of km.
>
> **REFERENCES**: Tarabukin and others, 1997; Rudenko and others, 1998.

## KPR Kyushu-Palau terrane (Island arc) (Paleocene) (Western Pacific Ocean)

Consists of Paleogene island arc volcanic rocks forming ridge that was
rifted away from the Izu-Bonin arc during opening of Shikoku basin in
Oligocene and Miocene. Ridge forms a linear escarpment up to 2000 m high
and bounded by normal faults along boundary between the Shikoku Basin
and ridge.

**REFERENCES**: Ingle and Karig, 1975; Shiki and others, 1984; Yamazaki
and Yuasa, 1998.

## KR Kara terrane (Continental margin turbidite) (Late Neoproterozoic) (northern part of Taimyr Peninsula)

## 

Extends in a northeastern direction for 700 km long and ranges up to 100
km wide. Consists chiefly of rhythmically alternating sandstone,
siltstone, and pelite, Riphean acritarchs, that was deposited along a
continental slope and foot. Terrane metamorphosed from low grade of
greenschist facies to amphibolite facies during intrusion autochthonous
granite and migmatite. Rb-Sr and K-Ar metamorphism isotopic age is 270
and 277 Ma. The U-Pb isotopic age of autochthonous granite is 306 Ma,
and Sm-Nd isotopic model age of the crust is 1.0-1.2 Ga. Terrane is
intruded by Permian two-mica and biotite-amphibole granite and
granodiorite along discordant contacts. Adjacent to the granites is a
distinct metamorphic zoning from unmetamorphosed rocks to muscovite and
amphibole hornfels facies. A U-Pb isotopic age of these granites and
granitoids is 264 Ma; Rb-Sr and Ar-Ar isotopic ages are 252-258 Ma, and
a Sm-Nd model age of the crust is 850-1075 Ma. Terrane is interpreted as
a microcontinent or passive margin of Kara paleocontinent.

**REFERENCES**: Makhlaev, Korobova, 1972; Zabiyaka, 1974; Bezzubtsev and
others, 1986; Uflyand and others, 1991; Vernikovsky and others, 1995,
1998; Vernikovsky, 1996.

## KRT Kurtushiba terrane (Accretionary wedge, type B) (Late Neoproterozoic and Early Cambrian) (Southern West Sayan)

## 

Consists of a Vendian-Early Cambrian accretionary wedge exposed in a
package of tectonic sheets that are thrust to the northwest over the
early Paleozoic continental margin turbidites of the West Sayan terrane.
Several tectonostratigraphic units are recognized. (1) An upper sheet of
7 km thickness occurs in the southeastern part of the terrane and
consists of a lower ophiolite section, locally disturbed, of
serpentinized harzburgite, banded dunite-harzburgite complex, gabbro, a
sheeted-dike diabase complex, and pillow lava and tuff. (2) Underlaying
is the sedimentary-volcanogenic part of the ophiolite with total
thickness over 5-6 km (Chingin suite). The lower part is mainly pillow
lava, tuff, diabase sills and dikes, and the upper part is siliceous
shale, graphite siliceous shale, shale, graywacke, and carbonate rocks.
A Vendian age is suggested by oncolite and catagraphite. Several sheets
of Early Cambrian island-arc rocks of andesite basalt, sandstone,
gravelstone, conglomerate, and limestone with archaeocyata (Tereshkin
suite) also occur. The volcanic rocks are characterized by low Ti and
Fe/Mg ratios and high Al. (3) Structurally below is a broken belt of
metamorphic schist that forms the northwestern margin of the terrane.
The matrix of metamorphic rocks consists of tuffaceous sedimentary rocks
with subordinate basalt (Akkol suite) and are the sedimentary part of
the Vendian-Early Cambrian accretionary wedge. The metamorphic schist
contains glaucophane, crossite and winchite. The metamorphic schist of
the Kurtushiba terrane may correlate with those of the Dzhebash and Amil
terranes.

Zones of serpentinitic melange separate the tectonic sheets of upper
ophiolite and metamorphic schist. The melange includes the clasts of
surrounding rocks, such as glaucophane schist, the lower ophiolite, and
exotic rocks including garnet amphibolite and limestone. The
Vendian-Early Cambrian units are structurally overlain by the Late
Silurian motley, shallow-water marine molasse with interlayered
limestone with brachiopods and corals. The molasse fills various
fault-bounded syncline structures. Within some depressions the Silurian
deposits are unconformably overlain by the Early Devonian continental
sedimentary-volcanogenic deposits. The terrane is interuded by Early
Devonian granitoid bodies that occur in the Late Silurian and Early
Devonian synclines.

**REFERENCES**: Zonenshain, 1963; Eremeev, Sibilev, 1969, 1974; Isakov,
Korobeinikov, 1970; Sobolev and Dobretsov, 1977; Kheraskov, 1979;
Melyakhovetsky and Sklyarov, 1985.

## KT Khemchik-Tapsa terrane (Accretionary wedge, type A) (Cambrian through Ordovician) (Tuva)

## 

Occurs along the northern margin of the Tannuola and Ondum island-arc
terranes and consists of the eastern Tapsa and western Khemchik parts.
The eastern Tapsa part consists of a tuffaceous siliceous-terrigenous
sequence, with flysch in the upper part (Tapsa and Bayankol suites). The
sequence contains olistostrome horizons with olistoliths of carbonate
rocks, and lesser volcanogenic, siliceous, and other sedimentary rocks.
Ophiolitic tectonic sheets also occur. The western Khamchik part occurs
in the core of ridge-like anticlines with complicated faults and is
overlain by Ordovician-Silurian deposits. The pre-Ordovician rocks occur
in odd tectonic lenses are associated with the following rock units for
which the stratigraphic section is not clear. (1) Fragments of an
ophiolitic section of possibly Vendian-Early Cambrian age containing
ultramafic rocks, basalt, and siliceous rocks. The fragments consist of
oceanic island basalt and small blocks of carbonate rocks; (2)
turbidites of variable grain size derived from basalt and siliceous
rocks; (3) Early Cambrian ophiolitic olistostromes; (4) tuffaceous
carbonate-terrigenous deposits with Early Cambrian trilobites and
archaeocyata; and (5) terrigenous deposits that vary from coarse-clastic
to sandy clay with horizons of polymictic olistostrome. The sandstone
and shale matrix of olistostromes contains Middle Cambrian trilobites.
The first four units are interpreted as part of an accretionary wedge;
the sixth unit is interpreted as a forearc basin. The forearc trough
deposits are underlain by the Ondum island arc terrane. In the western
part, the boundary between the forearc and volcanic arc units overlain
by middle and late Paleozoic deposits of the Tuva trough.

**REFERENCES**: Amgaian, 1971; Berzin, 1979; 1987; Bukharov, 1979.

## KTN Kaitanak terrane (Accretionary wedge, type B) (Early Paleozoic or older) (Southern Gorny Altai)

## 

Occurs in the Charysh-Terekta strike-slip fault zone and consists of two
packages. (1) The lower (northern) package consists of
high-pressure/low-temperature metamorphosed mafic volcanic rocks,
siliceous deposits, and sandstone-shale deposits (Uimon suite). The
high-pressure minerals are glaucophane, crossite, winchite, and
piedmontite. K-Ar isotopic ages are 455-400 Ma. And (2) overlying
ophiolitic sheets, forming erratic tectonic blocks that are separated by
serpentinitic melange zones. The sheets are composed of serpentinized
ultramafic rocks, gabbro, a sheeted-dike complex(?), siliceous rocks,
mafic volcanic rocks, and lesser metaterrigenous and carbonate rocks.
Unlike the lower package, the upper package is metamorphosed at
low-pressure. Terrane is intruded by small bodies of middle Paleozoic
granite of the Altai volcanic-plutonic belt.

**REFERENCES**: Duk, 1982; Dobretsov and others, 1991; Buslov, 1992,
1998.

## KU Kurai terrane (Island arc) (Early Cambrian) (Eastern Gorny Altai)

## 

Consists of tectonic sheets separated by the zones of serpentinitic
melange. Two Vendian-Early Cambrian sedimentary-volcanogenic units,
formed in two stages of island arc evolution, exist. (1) A primitive
island arc containing a rhyolite-basalt assemblage (Balkhash suite) that
is overlapped or partly laterally replaced by siliceous tuff,
volcanoclastic rocks, black shale, and carbonate rocks (Tydtueryk
suite). Island-arc tholeiitic basalt is characterized by low Ti, Al, K,
and P, low total alkalinity under Na dominating over K, and high Mg/Fe
ratio. Some volcanic rocks are compositionally close to boninite. The
unit is intruded by plagiogranite-gabbro-pyroxenite bodies of the
Meshtueryk complex. And (2) a normal island arc assemblage (Kurai suite)
unconformably overlying the first unit and consists of calc-alkaline
volcanic rocks (tuff, tephritoids, andesite, andesite basalt),
tuffaceous terrigenous, terrigenous and carbonate rocks with an Early
Cambrian fauna. The volcanic rocks are intruded by gabbro-diabase
(Tadjilin complex). Terrane is unconformably overlain by Early-Middle
Devonian volcanic-sedimentary units of the Altai volcanic-plutonic belt.

**REFERENCES**: Gusev, 1991; Simonov, 1991; Simonov and Kuznetsov, 1991;
Shokalsky and others, 1997.

## KUV Kuvai terrane (Accretionary wedge, type A) (Neoproterozoic) (Northwestern Eastern Sayan) 

## 

Occurs in the Main Fault strike-slip zone and ranges up to 30-40 km to
the northwest, narrows to the southeast, and splits into several
tectonic lenses. Chiefly composed of Late or Middle Riphean
volcanogenic, carbonate, and sanddy-shale metamorphosed to greenschist
facies (Kuvai series and analogues). The northwestern part of the
terrane is a fragment of the north-northwest-striking imbricated
volcanic arc, that is thrust over an adjacent west backarc(?)
sedimentary basin. The volcanic arc consists of mainly mafic lava and
pyroclastic rocks of with local siliceous and andesite volcanic rocks
(Kuvai and Kershul suites). The volcanogenic rocks are interlayered with
carbonaceous limestone and siliceous shale, indicating a relatively
deep-water environment. In the upper part this volcanic-sedimentary
sequence are lahars, motley and red tuff-breccia, and dolomite
interbeds, indicating shallow-water and continental deposition. Upward,
the Kuvai suite grades into dolomites and submarine-landslide rocks,
shallow-water sand-clay-carbonate sedimentary rocks (Angaloy suite) that
contains variable size clasts of limestone, dolomite and tuff.

Also occurring are terrigenous-shale sedimentary rocks including sandy
shale sequences with subordinate carbonate deposits (Urman suite), and
carbonate sequences with lesser sandy shale sedimentary rocks (Mana
suite). The sand-shale sequences range up to 2 km thick and consist of
fine-grained sandstone, siltstone, siliceous, carbonaceous-siliceous and
carbonaceous-siliceous-chlorite shale, and thin limestone.

Also occurring are carbonate sequences that range up to 1500 m thick and
consist of dark carbonaceous limestone, often with interlayered clay and
sand, and carbonaceous-siliceous-carbonate shale. Thin horizons of
submarine-landslide conglomerate with the clasts of host rocks or Kuvai
(Kershul) volcanic rocks occur locally.

In the southeastern part of the terrane are fragments of ophiolite and
various volcanogenic rocks. The ophiolite occurs in separate sheets and
boudins that are composed of serpentinized dunite, harzburgite, and a
layered lherzolite-wehrlite-pyroxenite-gabbro-diorite complex. The
volcanogenic deposits consist of low- and high-Ti tholeiitic metabasalt
and andesite-dacite (Inzhigei suite). Several blocks contain Late
Riphean or, possibly, Vendian-Early Cambrian carbonate deposits up to 3
to 4 km thick (Mirichun suite and analogues). Also present are numerous
layered and stock-like bodies of titaniferous gabbro-pyroxenite, gabbro
and gabbro-diabase (Lysan complex) and sporadic dike-like and lens-like
bodies of serpentinized ultramafic rocks (Akshep complex) that are
gabbro-pyroxenite cumulates. The Kuvai terrane includes pre-oceanic
rift-related, oceanic crust, and island-arc units, and exotic, lens-like
blocks of Archean-Proterozoic metamorphic rocks of which the largest is
the Kansk terrane. The smaller terranes, not shown in the map (Arzybei,
Dzhuglym and others), occur adjacent to the Derba terrane, and consist
of sialic fragments that were detached from the craton in the Riphean.
These fragments were accreted to the craton, together with other
tectonic units, during large early and middle Paleozoic displacements.

Intrusion of Cambrian (Malaya Biryusa complex) and Ordovician-Silurian
(Bugulma complex) gabbro and granite is interpreted as forming during
collisional events and strike-slip faulting. Early Devonian rifting is
interpreted as forming subalkaline granite and syenite (Ognit complex).
Terrane is covered by terrigenous-carbonate deposits of the Mana basin,
that is interpreted as the marginal continental facies of a Vendian
through Middle Cambrian back-arc basin, Cambrian-Ordovician continental
molasse, and Devonian continental rift sedimentary-volcanogenic units.

**REFERENCES**: Semikhatov, 1965; Berzin, 1967; Berzin, Gibsher,
Postnikov, 1982; Khomentovsky and others, 1978; 1980; Abramovich and
others, 1989; Yaroshevich and others, 1995.

## KV Kamyshovy terrane (Island arc) (Late Jurassic through Late Cretaceous) (Southern Russian Far East)

## 

Occurs on Sakhalin Island and consists chiefly of: (1) oceanic basalt
and chert with Late Jurassic to Early Cretaceous radiolarian; and (2) an
overlying thick sequence of mid-Cretaceous basalt, andesite, argillite,
sandstone, and conglomerate (Pobedinskaya sequence) that contain Albian
to Cenomanian Inoceramus.

**REFERENCES**: Geology of the U.S.S.R., Sakhalin Island, 1970;
Simanenko, 1986.

## KW Kwanmo terrane (Granulite-paragneiss) (Paleoproterozoic) (Korea)

## 

Consists of metamorphic rocks of the Mach'ollyong Supergroup including:
(1) Songjin Group composed of biotite-, sillimanite-, cordierite, and
garnet-gneiss and migmatite; (2) Pukdaech'on Group composed of marble
and dolomite marble with schist and migmatite interlayers; and (3)
Namdaech'on Group composed of micaceous schist and quartzite. The
Mach'ollyong Supergroup is intruded by Late Permian granite of the
Tumangang Complex, the Jurassic Daebu granite, and Late Cretaceous
Bulgugsa granite that are interpreted as forming in active continental
margins. Tertiary overlap assemblages consist of epicontinental
terrigenous deposits and volcanic rocks of the Ch'ilbosan and Myongchong
Groups.

**REFERENCES**: Geology of Korea, 1993.

## KY Kotel\'nyi terrane (Passive continental margin) (Late Neoproterozoic through Late Triassic) (Taimyr Peninsula) 

Consists of following units. (1) A Ordovician through Early
Carboniferous unit (several km thick) of shallow-marine limestone,
dolomite, coquina, marl, and limestone breccia of age that is
interlayered with local conglomerate, mudstone, siltstone, and
sandstone. Unit contains an abundant and diversified coral, ostracod,
brachiopod, and gastropod fauna similar to that of the Siberian
platform. (2) In the southwest part of the terrane are Late Devonian and
Early to Middle Carboniferous turbidites composed of deep-water
mudstone, siltstone, sandstone, and limestone. (3) In the northern and
central parts of the terrane are Early to Middle Carboniferous and Early
Triassic sedimentary rocks. The Carboniferous and Permian deposits
consist of thin conglomerate, siltstone, and sandstone beds. A
stratigraphic hiatus occurs at the base of the Triassic units. And (4)
an conformably overlying Jurassic unit (up to 2000 m thick) of black
shale that contains interlayered fossiliferous limestone with
pelecypods, ammonites, foraminifers, crinoids, wood detritus, plant
spores, and pollen. The southern part of the terrane contains only Late
Triassic units and relationships with the Paleozoic units are not clear.
Recent studies suggest that thrusts may be widespread and that the
Paleozoic units structurally overly Mesozoic units (G. Aulov, written
commun., 1992). The Paleozoic and Mesozoic deposits are codeformed into
northwest-trending folds with steep axial surfaces. The age of folding
is interpreted as Carboniferous. Postaccretionary units consist of: (1)
Jurassic overlap units revealed by drilling in the Fadeev and Novaya
Sibir\' Islands; and (2) unconformably overlying, flat-lying Aptian
mudstone, siltstone, sandstone, silicic tuff, and coal, and Late
Cretaceous dacite. Aeromagnetic data indicate abundant mafic and
ultramafic plutonic rocks at depth. The southwest boundary of the
terrane is drawn along a linear positive gravity anomaly between the
Kotel\'nyi and Stolbovoy Islands (L.A. Savostin, written commun., 1992).
The eastern boundary of the terrane is defined from geophysical data
that imply a late Paleozoic and Mesozoic sequence (3 to 5 km thick) of
clastic deposits.

**REFERENCES**: Zhizhina, 1959; Volnov and others, 1970; Churkin, 1973;
Vinogradov and others, 1974; Volnov, 1975; Kos\'ko, 1977; Avetisov,
1983; Kos\'ko and others, 1990; Fujita and Cook, 1990.

## KZ Kuzeev terrane (Granulite-orthogneiss) (Paleoproterozoic) (Yenisey Ridge)

Occurs in elongated submeridional-trending plates in the central part of
the South Yenisey Ridge with a length of 200 km and ranging up to 30-40
km wide. Consists mainly two-pyroxene-plagioclase gneiss, metamorphosed
gabbro-norite, mafic schist derived from andesite and basalt, and local
charnockite. High-aluminous biotite-garnet gneiss derived from primarily
pelite and psammite sedimentary rocks. The Zemoveynyi massif contains
the largest group of gabbro-norite. Terrane was metamorphosed to
granulite facies. U-Pb zircon isotopic studies indicate a metamorphic
age of 1840 to 1920 Ma ().

**REFERENCES**: Zhizhina, 1959; Volnov and others, 1970; Churkin, 1973;
Vinogradov and others, 1974; Volnov, 1975; Kos\'ko, 1977; Volobuev and
others, 1980; Avetisov, 1982; Fujita and Cook, 1990; Kos\'ko and others,
1990; Bibikova and others, 1993.

## LA Laoling terrane (Island arc) (Late Ordovician through Silurian) (Northeastern China)

## 

Consists chiefly of (1) Late Ordovician metamorphic marine deposits and
siliceous volcanic-volcaniclastic rocks (over 2,000 m thick)
metamorphosed to quartz schist, mica-schist, metamorphic
intermediate-siliceous volcanic rocks, marble, slate and sandstone
(Shifen Formation) with *Sinkiangolasma, Leolasma and Rouscria*. (2)
Early Silurian volcaniclastic deposits and sedimentary rocks (over 3000
m thick) metamorphosed to slate, siltstone, phyllite, tuff, siliceous
lava, and sandstone (Taoshan Formation) abundent graptolites. (3) Middle
Silurian sandstone, siltstone and tuff (Zhangjiatun Formation), Late
Silurian shale, siltstone, graywacke and limestone (Erdaogou Formation);
and (4) local unconformably overlapping Middle Devonian limestone,
siltstone, limestone and sandstone (Wangjiajie Formation), and local
unconformably overlapping Carboniferous and Permian sedimentary rocks
and Mesozoic and Cenozoic sedimentary rocks. Terrane is intruded by
Silurian plutons and Hercynian plutons with a K-Ar isotopic age of 408
Ma. Terrane is strongly discontinuously latitudinal stretching and
intensely deformed by widespread, mainly Hercynian plutons. Faults
bounding terrane are covered.

**REFERENCES**: Tang Kedong and others, 1995; Zhao Chunjin and others,
1996; Bureau of Geology and Mineral Resources of JilinProvince 1989; Sun
Jiapeng and others, 2000.

## LG Laoyeling-Grodekov superterrane (Island arc) (Late Carboniferous and Permian) (Northeastern China, Southern Russian Far East)

## 

In northeastern China consists chiefly of: (1) discontinuous Early
Silurian sedimentary and volcaniclastic rocks composed of tuff, chert,
shale, slate, and siltstone that are intruded by Silurian plutons; (2)
Late Carboniferous(?) and Early and Late Permian carbonate, terrigenous
and intermediate-felsic volcanic, and volcaniclastic rocks, (Qinggouzi,
Kedao, Miaoling, Dashangou, and Shanxiuling Formations) composed of
limestone, siltstone, sandstone, conglomerate, tuff, rhyolite,
andescite; and (3) Mesozoic and Cenozoic overlap sedimentary
assemblages. Terrane is strongly intruded by Late Permian plutons.
Terrane strike approximately east-west. Western boundary not well
exposed.

**REFERENCES**: Zhang Qinglong and others 1989, 1996; Zhao Chunjin and
others, 1996; Khanchuk, A.I. and others, 1996; Jilin GMRB, 1989; Tang
Kedong and others, 1995; Sun Jiapeng and others, 2000.

In Russian Southeast, consists chiefly of the following units. (1) A
lower tectonic melange unit contains fragments of Early Silurian
granite-pebble-bearing conglomerate, sandstone, siliceous mudstone and
lesser interbedded basalt, andesite, rhyolite, and tuff. Sedimentary
rocks locally contain brachiopods and graptolites, and are locally
intensely deformed and metamorphosed to middle amphibolite facies. The
melange structural thickness is about 1,500 m. And (2) an upper unit
contains Permian basalt, andesite, rhyolite, conglomerate, sandstone,
mudstone, and shale, and lesser interbedded limestone lenses with Late
Permian Tethyan fusulinids. The structural thickness is about several
thousand meters. Permian rocks are intruded by zoned
dunite-clinopyroxenite-gabbro intrusions that form Alaskan-type plutons,
and local tonalite and plagiogranite. Permian igneous rocks are
interpreted as part of a Permian volcanic arc. Younger,
collision-related, Late Permian granitic plutons intrude the terrane and
are co-magmatic with Permian volcanic rocks in the Khanka superterrane.
This relation suggests that accretion of the Laoelin-Grodekovsk terrane
and Khanka superterrane occurred at the end of the Paleozoic. The
Laoelin-Grodekovsk terrane is overlapped by: (1) Triassic plant-bearing
conglomerate and sandstone; and (2) to the west in China by Late
Triassic continental rhyolite, Late Jurassic rhyolite, and Late Jurassic
subduction-related granitic plutons.

**REFERENCES**: Evlanov, 1971; Shcheka and others, 1973; Nazarenko and
Bazhanov, 1986; Izosov and others, 1988; Khanchuk and others, 1988.

## LK Lake terrane (Island arc) (Late Neoproterozoic and Cambrian) (Western Mongolia)

## 

Occurs vast areas of the Valley of Lakes and foothills of Mongolian
Altay and Hangay Mountain Range in western Mongolia. Extends for 1000 km
and ranges up to 200 km wide. Consists of Late Precambrian to Cambrian
Troodos-type ophiolites, island arc and backarc basin
volcanic-sedimentary rocks, and plutonic rocks of different
compositions. The well-known intact Han Tayshir ophiolite contains
Alpine-type ultramafic rocks, a layered mafic complex, an upper gabbro
unit, sheeted dikes, basalt pillow lava, and deep marine siliceous
sedimentary rocks. A plagiogranite U-Pb zircon age is 568±4 Ma. The
island arc rocks include calc-alkalic volcanic rocks, reef limestone,
graywacke, and olistostrome of the Late Vendian to Amgin stage of the
Early Cambrian. A basalt Sm-Nd isotopic age is 522± 13Ma. The island arc
complex contains small intrusions and sills of layered gabbro with Sm-Nd
isotopic ages of 527 to 531Ma (Kovalenko and others, 1996, and is
intruded by Middle Cambrian(?) I-type granite of the Togtohynshil
complex. Terrane is moderately to intensely folded and thrust faulted,
and contains melange, olistostomes, and large allochthonous ophiolites
including the Taishir, Naran, Bayannuru, and and ophiolites. Terrane is
overlain by Ordovician, Silurian marine sedimentary rocks, Devonian
volcanic rocks, Early Carboniferous marine sedimentary rocks, and Permia
and Jurassic non-marine deposits. A stitching complex is a Middle to
Late Cambrian S-type granite. Terrane is interpreted as a Vendian and
Cambrian island arc system that contained several island arc, backarc,
and forarc basin units.

**REFERENCES**: Zonenshain and Kuzmin, 1976; Zonenshain and Kuzmin,
1976; Dergunov, 1989; Tomurtogoo, 1989, 1997, Rhuzentsev and
Burashnikov, 1995; Khain and others, 1994; Kovalenko and others, 1996;
Windley and others, 2000.

## LN Lan terrane (Continental margin turbidite) (Devonian through Triassic) (Southern Russian Far East)

## 

Consists chiefly of Middle Devonian, Carboniferous, Permian, and
Triassic turbidites with olistostrome horizons (Dzhegdalinsk,
Ustarteksk, Arteksk, Torbosk, Alukansk, Lansk, and Deloesk suites).
Inclusions in the olistostromes consist of mafic volcanic rocks, chert,
and limestone. Major olistostrome units are: (1) a Middle Devonian
olistostrome composed of limestone with Early Cambrian archaeocyatheans
with North Asian platform affinity; (2) the Late Carboniferous Alukansk
suite of spilite, diabase, sandstone, and silicic volcanic that in
interpreted as forming adjacent to a volcanic island arc; and (3) a Late
Triassic olistostrome that contains Triassic fossils that are exotic to
the Russian Southeast. The Middle Devonian, Visean-Moscovian, and Late
Permian macrofossils of the terrane constitute a Boreal fauna. The Late
Permian unit contains a Boreal fauna contrasts sharply with the
Tukuringra-Dzhagdi terrane that contains a Tethyan fauna. Overlapping
the Lan terrane are Early and Middle Jurassic shallow-marine clastic
rocks and tuff that also overlap the Baladek terrane. Regional tectonic
analysis suggests that these Jurassic deposits formed in the forearc
basin of the Uda volcanic-plutonic belt that occurs along the Stanovoy
block of the North Asian craton.

**REFERENCES**: Kirillova and Turbin, 1979, Brudnitskaya, 1990.

## MB Mogen-Buren terrane (Oceanic) (Late Neoproterozoic and Early Cambrian) (Southeastern Gorny Altai)

## 

Consists of Vendian and Early Cambrian volcanic-sedimentary rocks
metamorphosed to greenschist facies. The lower horizons consist of
greenstone volcanic rocks and tuff with subordinate terrigenous rocks,
and local serpentinite and gabbro. The upper horizons are composed
chiefly of terrigenous and tuffaceous terrigenous rocks. The lower part
of the terrane is interpreted as forming in an oceanic environment,
whereas the upper is interpreted as forming in a fore-arc environment.
Terrane intruded by early Paleozoic subalkaline granite and middle
Paleozoic alkaline and plumasite granite. Terrane bordered by
imbricated-thrust structures and strike-slip faults, and is interpreted
as a series of turbidite and related deposits that formed along an early
Paleozoic continental margin.

**REFERENCES**: Dergunov, 1967; Avrov , 1980.

## MC Mino Tamba Chichibu terrane (Accretionary wedge, type B) (Permian through Early Cretaceous) (Japan)

## 

Consists chiefly of sandstone, mudstone, siliceous shale, chert,
limestone, and basalt. Sandstone, mudstone, and siliceous shale are of
Jurassic are Cretaceous. Chert includes radiolarians ranging from
Permian to Early Jurassic age. Limestone yields Carboniferous to Permian
fusulinids and is intimately associated with pillow basalt. The various
lithologies are interpreted as derived from oceanic crust ranging in age
from Carboniferous to Early Cretaceous that were iincorporated into a
melange. Terrane was amalgamated with Hida terrane in middle Cretaceous.
Both termanes are unconformably overlain by Cretaceous felsic volcanic
rocks and are intruded by Late Cretaceous to Paleogene granite.

**REFERENCES:** Wakita, 1988; Adachi and others, 1992.

## MG Magan terrane (Tonalite- trondhjemite-gneiss) (Paleoproterozoic) (Yakutia)

## 

Consists of a lower structural unit of homogeneous biotite and
biotite-amphibole orthogneiss derived from
tonalite-granodiorite-adamellite composition, and an upper structural
unit of garnet-bearing and highly aluminous gneiss and carbonate rocks
(Late Anabar Group). The tonalite-granodiorite-adamellite complex is
similar to the Amitsok augen gneiss and Uivak II gneiss. Average Sm-Nd
model age for the Magan terrane substratum is 2.94[+]{.underline}0.09
Ga. Terranne metamorphosed to granulite facies. Terrane characterized by
poorly-defined structures, a mosaic magnetic field, and very low gravity
anomaly values relative to the neighbouring terranes.

**REFERENCES**: Vishnevskiy, 1978; Oxman, 1989; Lutz and Oxman, 1990;
Rosen and others, 1999.

## MK Malokhingansk terrane (Accretionary wedge, type B) (Neoproterozoic and Cambrian) (Western part of Russian Southeast)

## 

Consists chiefly of the Neoproterozoic and Early Cambrian units that
form a continuous sequence of shale, siliceous schist, chert, and
limestone (Ditursk, Iginchinsk, Murandavsk, Rudnosnsk, and Londokovsk
Suites). The Neoproterozoic and Cambrian rocks are zonally metamorphosed
from green shale to amphibolite faces. Cherts include interlayers of
oceanic ferromanganese and manganese minerals. The Neoproterozoic and
Cambrian sequence is intruded by granitic rock of the Birsk and
Birobidzhan Complexes that yield K-Ar isotopic ages of 301 Ma.
Uncomformably overlying, post-accretion units are Devonian, Permian, and
Triassic shallow-marine, clastic rocks, including Devonian limestone in
the Niransk, Pachansk, and Osakhitinsk Suites. The clastic rocks were
deposited in a narrow, fault-bounded belt along southeastern boundary of
the terrane, and contain abundant fauna that is similar to other zones
of Central Asia. The Permian Osakhinsk Suite contain Kolyma Boreal
pelcypods whereas the Permian deposits of the Badzhal terrane contains
Tethyan fusulinids. Various Jurassic clastic units, which formed in
individual basins, overlap the terrane. Overlapping the Malokhingansk,
Badzhal, Ulban, and Nilan terranes is the Cretaceous Khingan-Okhotsk
volcanic-plutonic belt (unit ko).

**REFERENCES**: Krasny, 1966, Martynyuk and others, 1983; Kozlovsky,
1988.

## MM Mamyn terrane (Passive continental margin) (Archean?) (Southern Russian Far East)

## 

Consists chiefly of two major metamorphic units. (1) an older Early
Archean(?) unit that consists of garnet-cordierite-sillimanite gneiss
and schist, granite-gneiss, gabbro, and amphibolite metamorphosed to
granulite facies; and (2) an assumed younger sequence of Proterozoic(?)
greenschist, metasandstone, marble, quartzite, felsite, sandstone, and
siltstone. Metamorphic units are poorly exposed among the extensive
Paleozoic granitic rocks of the Kiviliysk complex that have a minimum
K-Ar isotopic age of 495 Ma. Overlapping the metamorphic rocks of the
terrane are: (1) Early Cambrian limestone and dolomite with
archaeocyathids and Silurian clastic rocks (Mamynsk suite), and abundant
quartz-rich sandstone and siltstone; (2) Middle Devonian siltstone,
sandstone, and limestone (Oldoisk and Imchansk suites) that, along with
the Silurian units, are gently folded; (3) Early Cretaceous volcanic
rocks (Peremykinsk and Taldansk suites) of the Umlekan-Ogodzhin
volcanic-plutonic belt; and (4) terrestrial clastic rocks of the Amur
sedimentary basin. These overlap assemblages link together the Mamyn,
Gonzha, Oldoi, and Turan terranes.

**REFERENCES:** Shilo, 1982, Kozlovsky, 1988.

## MN Mandah terrane (Accretionary wedge, type A) (Devonian) (Southern Mongolia)

## 

Occurs in narrow, fault-bounded lens, between the Gurvansayhan and
Mandalovoo and consists chiefly of a strongly folded and faulted
assemblage of undated metavolcanic and metasedimentary rocks, and
melange containing blocks of basalt, andesite, tuff, Devonian
coral-bearing limestone, minor amphibolit, and gabbro. Matrix for the
melange contains mainly sheared serpentinite, and fine-grained sandstone
and siltstone, and locally contains olistostrome with blocks of
limestone and sandstone. Postaccretionary complex are Middle to Late
Carboniferous volcanic-plutonic rocks. Terrane is interpreted as an
accretionary wedge that was tectonically paired to the Gurvansayhan arc
terrane.

**REFERENCES**: Suetenko, 1973; Tomurtogoo, 1984, Ruzhentsev and others,
1985.

## MO Mandalovoo-Onor terrane (Island arc) (Middle Ordovician through Early Carboniferous) (Southern Mongolia, Northeastern China)

In Mongolia, forms a narrow up to 50 km wide, about 1800 km long belt in
northern margin of southern Mongolia. Consists of a complexly-deformed,
but partly coherent, long-lived stratigraphic succession of : (1) Middle
to Late Ordovician sandstone, siltstone, minor conglomerate, and lenses
of limestone with corals and brachiopods; (2) Silurian sandstone,
siltstone, argillte, minor conglomerate, massive limestone with corals
and brachiopods including Tuvaella fauna of Siberian affinity; (3) Early
Devonian conglomerate, sandstone, and minor felsic tuff; (4) Early to
Middle Devonian fossil-rich limestone, sandstone, and ash tuff; (5)
Middle to Late Devonian massive and pillow basalt, andesite basalt,
andesite, rhyolite, tuff, volcaniclastic sandstone, siltstone, chert
with radiolarians and conodonts, and sparse limestone with brachiopods
and corals; and (6) Early Carboniferous sandstone, siltstone, chert, and
tuff that contains conodonts and megafossils. Spiderdiagrams for the
Devonian basalt display a pattern that most similar to volcanic arc
basalt. Preaccretionary granitic rocks include Middle to Late Devonian
small plutons of diorite and granodiorite. Terrane is overlain by Middle
to Late Carboniferous, Early Permian volcanic rocks (unit mn), Late
Permian sedimentary rocks, and Early Cretaceous volcanic rocks.
Stitching complexes include Middle to Late Carboniferous and Early
Permian granite. Provenance data from the Ordovician and Silurian
sandstone suggested that the source material for these sandstone may
have been either an uplifted continental block or the eroded, exposed
roots of volcanic arc. Paleomagnetic determinations from Devonian
andesite basalt suggest about 40^0^ northward motion and 75^0^ clockwise
rotation. Terrane is interpreted as a displaced fragment of a Devonian
island arc that is underlain by thick sedimentary rocks derived from an
older island arc.

**REFERENCES:** Suetenko and others, 1977; Ruzhentsev and others, 1987;
1984, Badarch, 1990; Voznesenskaya and Badarch; 1991, Didenko, 1992;
Lamb and Badarch, 1997, 2001.

In northeastern China, terrane extends in a northeast direction and
consists of: (1) slate, phyllite, metatuffaceous siltstone,
metatuffaceous sandstone, and metasandstone with trilobites,
brachiopods, and anthozoa; (2) late Silurian metasandstone, slate and
limestone with Gondwana brachiopods; (3) overlapping Devonian strata
containing radiolaria, brachiopods, anthozoa, and marine fossils, chert,
spilite, keratophyre, quartz keratophyre, andesite basalt and the
terrigenous clastic rocks with intercalated intermediate-siliceous
volcanic rocks with Early Carboniferous marine and limnic fossils.
Terrane intruded by syntectonic ultramafic and granitic plutons with
Rb-Sr isotopic age of 354 Ma. Terrane unconformably overlapped by
Permian volcanic rocks and terrigenous clastic rocks.

**REFERENCES:** Bureau of Geology and Mineral Resources of Inner
Mongolian, 1991; Bureau of Geology and Mineral Resources of
Heilongjiang, 1993; Ye Mao, 1994; Xu Wenliang, 1994.

## MR Maralikha terrane (Accretionary wedge, type A) (Middle Devonian or older) (Northwestern Gorny Altai)

## 

Consists of a monotonous unit (Maralikha suite) (over 3 km thick) of
gray and greenish fine-grained sandstone, siltstone, and
sericite-siliceous shale that are generally finely and rhythmically
interbedded, and several boudins of marble-like limestone with crinoids.
The limestone may be part of the sandy shale deposits, or olistoliths.
Hosting the carbonate lenses are possibly distal facies turbidites.
Terrane is intruded by Late Devonian calc-alkaline and plumasite granite
with U-Pb zircon ages of 362 to 371 Ma, and by Late Permian and Early
Triassic REE granite. Terrane is overlapped by Cenozoic deposits of the
West Siberian sedimentary basin.

**REFERENCES**: Iwata, and others, 1997; Vladimirov and others, 1997.

## MS Muya terrane (Metamorphic) (Late Archean? and Paleoproterozoic?) (Transbaikalia)

## 

Southern part of terrane contains an Early Archean metamorphic complex
(Kindikansky series) consisting of amphibole-, garnet-amphibole-,
biotite-amphibole-, and garnet-biotite- (with hyperstene, diopside,
disthen, sillimanite) gneiss and schist with contains lenses of garnet
ultramafic rocks and eclogite. These units display relatively older
high-pressure stage, and relatively younger diaphtoric metamorphisms. In
the central part of the terrane, with a unclear relatin, the Late
Archean Ileirsky and Ljunkutsky suites contain gneiss and schist with
clinopyroxene, plagioclase, hornblende, garnet and biotite metamorphosed
to eclogite facies, and two younger diaphtoric stages. In the northern
part of terrane, the Ileirsky contains gneiss and schist with garnet,
mica and hornblende, amphibolite and marble, and lenticular bodies of
eclogite. Outcrops are controlled by blastomylonite zones and overthrust
slabs with Sm-Nd rock and minerals isochron ages of 653 Ma ago. Seismic
data suggest these units form a large slab that gently dips northeast to
a depth 20 km.

In the northern part of the terrane, the Ileirsky suite is concordantly
overlapped by gneiss, schist, and marble of the Ljunkutsky suite. Both
are metamorphosed to garnet-kyanite-biotite-orthoclase and
garnet-sillimanite-biotite-orthoclase subfacies, with younger
diapthorisis at greenschist facies conditions. The Ljunkutsky suite is
unconformably overlain by the PaleoproterozoicParamsky series containing
carbonate-terrigenous rocks that are metamorphosed to greeschist facies
conditions. Terrane is intruded by Paleoproterozoic(?) granite bodies of
the Ileirsky complex and deformed into as folds with northeastern to
submeridional strikes. In the Riphean the Muya terrane was a massif with
relatively rigid internal structural framework. Accretion of the Muya
terrane and the adjacent Riphean island arc terrane to the craton is
interpreted as occuring in the Riphean with formation of granite bodies
with Nd-Sm isotopoic model ages of 789 and 784 Ma. The terrane is
overlapped by Vendian-Cambrian terrigenous-carbonate sedimentary rocks
of the Upper Angara sedimentary basin, and is intruded late Paleozoic
granite batholiths.

**REFERENCES**: Bolonev and others, 1983; Bulgatov 1983, 1988; Bozhko
and others, 1999; Dobretsov and others, 1989; Doronina, Sklyarov, 1995;
Shatsky and others, 1996; Rytsk and others, 1999.

## MT Matveevka terrane (Metamorphic) (Archean? or Proterozoic?) (Southern Russian Far East)

## 

Occurs north of Lake Khanka consists of Precambrian crystalline rocks:
(1) diopside-calcite, less common forsterite-calcite, and
calcite-dolomite graphite-bearing marble interlayered with gneiss
(Ruzhinsk Formation, over 1000 m thick) at the base of visible section;
overlying biotite-sillimanite and garnet-biotite-cordierite gneiss, and
hypersthene-magnetite and fayalite quartzite interlayered with marble
(Matveevsk Formation, about 3000 m thick) with a moderate pressure
assemblage of garnet-cordierite and orthoclase-biotite; and (3) an
section of biotite-amphibole schist and gneiss, amphibolite, and marble
(Turgenevsk Formation, about 4300 m thick).

**REFERENCES**: Khanchuk and others, 1996.

## NA Nadanhada terrane (Accretionary wedge, type B) (Middle Triassic through Middle Jurassic) (Northeastern China)

## 

Consists chiefly of: (1) Middle and Late Triassic pelagic chert with
*pseudoheliodiscus* and pillow lava; (2) Early and Middle Jurassic
pelite and siliceous mudstone; (3) Late Jurassic turbidite deposits; and
(4) unconformbly overlying Late Jurassic and Early Cretaceous sandstone
and mudstone with *Buchia*.

**REFERENCES**: Zhang Qinglong and others, 1989; Shao Jian and others,
1991, 1992; Tang Kedong and others, 1995; Khanchuk and others, 1996; Sun
Jiapeng and others, 2000.

## NAB Nabilsky terrane (Accretionary wedge, type B) (Late Cretaceous through Paleogene) (Southern Russian Far East)

## 

Consists chiefly of a melange unit with a matrix of late Campanian to
early Paleogene(?) turbidite and Campanian chert olistostromes that
enclose bodies of Late Jurassic and Early Cretaceous radiolarian chert
and basalt and guyot fragments. Guyots are capped by Late Jurassic to
Early Cretaceous limestone that contains Tethyan reef corals. The
melange also locally contains ophiolitic fragments, including large
harzburgite and lherzolite bodies, and sparse cumulative gabbro and
sheeted dikes. Geochemical data indicate both MORB and seamount basalt
occurs in melange. The southern part of the terrane also include a large
allochthon (1.5 x 8 km) that consists of medium-grade metamorphic rocks
with K-Ar white mica ages of 130 to 148 Ma. The Nabilsky terrane is
tectonically linked to the East-Sikhote-Alin volcanic-plutonic belt.

**REFERENCES**: Geology of the U.S.S.R., Sakhalin Island, 1970;
Raznitsin, 1982; Rozhdestvensky, 1983; Rikhter, 1986; Khanchuk and
others, 1988.

## ND Nora-Sukhotin-Duobaoshan terrane (Island arc) (Neoproterozoic through Early Carboniferous) (Mongolia, Northeastern China, Russian Far East)

## 

In eastern Mongolia, forms a narrow northwest-trending belt in Mongolia
and consists of: (1) Middle and Late Riphean(?) gneiss, schist,
stromatolitic marble, and limestone; (2) Early and Middle Cambrian
sandstone, siltstone, minor conglomerate, and olistostrome; (3) Middle
to Late Ordovician sandstone, siltstone, phyllite, minor conglomerate,
and limestone with corals; (4) Silurian sandstone, siltstone, argillite,
minor coral-bearing limestone; and (5) thick Early to Middle Devonian
sandstone, siltstone, argillite, minor basalt, andesite, tuff,
conglomerate, and limestone with brachiopods and corals. Units (1-4) are
metamorphosed to greenschist facies and contain disrupted lenses of
serpentinite and gabbro.Terrane is intruded by Silurian granite and
granodiorite, and minor quartz diorite with K-Ar isotopic ages of 419 to
435 Ma. Terrane overlain by Early Carboniferous shallow-marine
sedimentary rocks, Middle to Late Carboniferous and Permian subalkalic
and alkalic volcanic and volcaniclastic rocks, and stitched by Middle to
Late Carboniferous and Permian granite and leucogranite, and Triassic
and Early Jurassic REE granite. Terrane is correlated with the Dong
Ujumqin belt and interpreted as an early Paleozoic active continental
margin or island arc.

**REFERENCES:** Geology MPR, 1973; Tang, 1990; Hsu and others, 1991,
Badarch and Orolmaa, 1998.

In Northeast China, consists of: (1) Cambrian metasandstone and phyllite
with intercalated, lenticular limestone; (2) Ordovician and Silurian
metabasalt, metaandesite, metadacite, and volcanic breccia with the
intercalated marble; (3) Early Devonian shale, tuff, spilitic
keratophyre; and (4) Middle and Late Devonian sandstone, shale, and
limestone. Terrane is overlapped by Lower Carboniferous molasse
formation with fossils and flora. Terrane intruded by subduction-related
granodiorite and adamellite in the Late Carboniferous.

**REFERENCES**: Xie Guolun, 1980; Cui Ge, 1983; Bureau of Geology and
Mineral Resources of Heilongjiang Province, 1993; Zhang Dequan, 1998.

In Russian Southeast, occurs in a mostly concealed region beneath
Cenozoic sedimentary rocks of the Amur-Zersk basin and stratigraphic
sequence reconstructed from isolated outcrops. Consists of two units:
(1) mafic greenstone, mica schist, marble, metasandstone, and quartzite
(Dagmarsk and Neklinsk suites) of presumed Neoproterozoic to early
Paleozoic age, with greenschist-facies metamorphism; and (2) several
sequences of Silurian through Early Carboniferous andesite, sandstone,
siltstone, greenschist, limestone, conglomerate, shale, and diabase that
locally are variably metamorphosed to greenschist facies. The Late
Silurian through Early Carboniferous units contain a marine fauna and an
Angara flora. Terrane is unconformably overlapped by Permian sandstone,
shale, conglomerate, tuff, and intermediate volcanic rocks that contain
an Angara flora. The unconformity postdates the late Paleozoic
amalgamation of the Nora-Sukhotin terrane with the Bureya superterrane.
The Nora-Sukhotin terrane is interpreted as a middle Paleozoic island
arc that formed on an older metamorphosed accretionary wedge complex.

**REFERENCES**: Sorokin, 1972; Shilo, 1982; Martynyuk, 1983.

## NK Nakhimovka terrane (Metamorphic) (Archean? or Proterozoic?) (Southern Russian Far East)

## 

Occurs north of Lake Khanka and consists of Precambrian crystalline
rocks: (1) biotite- and biotite-amphibole gneiss with lenses of marble
and amphibolite occur at the lower part of the section (Nakhimovsk
Formation, over 1000 m thick); and (2) overlying biotite-, diopside-,
and muscovite-graphite schist (Tatyanovsk Formation, about 2500 m).

**REFERENCE**: Khanchuk and others, 1996.

## NL Nilan terrane (Accretionary wedge, type B) (Devonian through Permian) (Southern Russian Far East)

## 

Terrane consists of a series of nappes and composed of: (1)
tectonically-mixed Missisipian and Early Pennsylvanian deep-marine
siliceous and hemipelagic sedimentary and volcanic deposits; (2) Early
Devonian, Middle Pennsylvanian and Permian turbidite and basalt; (3) in
the western part of the terrane, intensely metamorphosed middle and late
Paleozoic rocks; Paleozoic(?) gabbro, gabbro-amphibolite (Zlatoustovsk
complex), and late Paleozoic quartz diorite, granodiorite, and
plagiogranite (Ingagli complex) a K-Ar isotopic age of 235-230 Ma.
Overlapping sedimentary, volcanic-sedimentary assemblages, and stitching
plutonic assemblages are: (1) Early Cretaceous granitoids (Kharga
complex), and andesite (Umlekan-Ogodzhin volcanic-plutonic belt); (2)
Late Cretaceous granitoids and siliceous volcanic rocks of
Khingan-Okhotsk volcanic-plutonic belt; and (3) Neogene and Quaternary
non-marine clastic deposits and basalt.

**REFERENCES**: Martynyuk and others, 1990; Krasni and others, 1996.

## NN Nankai terrane (Accretionary wedge, type A) (Miocene through Quaternary) (Western Pacific Ocean, Central Japan)

## 

Consists of sandstone, mudstone, and conglomerate and is subdivided into
an accretionary prism and forearc basin deposits. Accretionary prism
formed by the subduction of the Philippines Sea Plate along the Nankai
trough, and thick forearc basin strata (Miura Group) were deposited
during the Miocene to early Pliocene. The Nankai terrane also includes
Quarternary trench fill sedimentary rocks that consist of turbidite and
hemi-pelagic mudstone. Terrane contains a large number of active thrusts
that parallel are to strike of trench and that dip gently towards
Japanese islands arc. The thickness of sedimentary rocks in Nankai
Trough ranges from 500 m to 2,000 m. Rate of convergence ranges from 3
to 4 cm per year. The age of subducting oceanic plate ranges from 15 to
30 Ma.

**REFERENCES**: Ogawa and Taniguchi, 1988; Wakita and others, 1992;
Hanamura and Ogawa, 1993.

## NO North Margin terrane (Accretionary wedge, type B) (Carboniferous and Early Permian) (Northeastern China)

## 

Consists chiefly of: (1) pillow lava and ultramafic rocks; (2) a western
part of mainly carbonate and silicate interlayered siliceous shale; and
(3) an eastern part of turbidite and olistostromal deposits. Turbidte is
derived from both granitic and ophiolite units and contains microfossils
of *Monodiexodina, Verbeekina and Kahlerina,* and plant fossils of
*Emplectopteris triangularis and Taeniopteris*. Terrane is deformed by
appressed folds and thrust faults and intruded by Late Permian and Late
Jurassic granitic plutons. Terrane is interpreted as an accretionary
wedge that was tectonically accretionary to the Laoling terrane.

**REFERENCES**: Bureau of Geology and Mineral Resources of Jilin 1989;
Guo Shenzhe and others, 1992; Shao Jian and others, 1995; Tang Kedong
and others, 1995; Krasnyi, L.I.and others, 1996; Zhao Chunjin and
others, 1996; Sun Jiapeng and others, 2000.

## NR Nechera terrane (Granulite-paragneiss) (Archean(?) and Proterozoic) (Transbaikalia)

## 

Consists Archean units of: (1) a lower unit of hypersthene-, amphibole-,
biotite-, and garnet-gneiss and schist with minor enderbite and
charnockite (Chepoksky suite of the Nechera series) that exhibit
amphibolite facies diaphtoresis; (2) concordantly overlying biotite-,
garnet-biotite-, and amphibole-biotite plagiogneiss with layers of
crystalline marble calciphyres, and quartzite metamorphosed, all
metamorphosed to amphibolite facies (Olongdisnky suite); (3)
Paleoproterozoic Ilinaksky suite (Kevaktinsky series) composed of
quartzite, metasandstone, plagiogneiss, micaceous; and
graphite-cordierite schist; and (4) Paleoproterozoic Khodokansky suite
(Kevaktinsky series) composed of metasandstone, metaaleurolite, and
carbonaceous-micaceous schist. Units (3-4) are metamorphosed to biotite
and garnet zones, locally to staurolite zone. Intruding these units are
granitoids of the Chuya-Nechera complex with U-Pb zircon ages of 1850 Ma
and 2114 Ma, and Early Riphean(?) gabbro-diabase and diabase dikes.
Metamorphic rocks are multiply deformed with sparse relic
Paleoproterozoic domal structures. During Intruding during Late Riphean
accretion of cratonal and Riphean terranes to the North Asian Craton
were stocks and dikes and granite porphyry and granodiorite-poprhyry
(Yazovsky complex) with a U-Pb zircon age 730 of Ma. Post-accretionary
granite batholiths (Konkudero-Mamakan complex) have U-Pb zircon ages of
350-300 Ma.

**REFERENCES**: Neimark and others, 1990; Bukharov and others, 1992;
Ivanov and others, 1995.

## NRS North Sayan terrane (Island arc) (Neoproterozoic through Early Cambrian) (Northwestern Sayan)

## 

Terrane exhibits a complicated structure and consists of tectonic
blocks, lenses, and sheets. Four units are recognized. (1) The
Kizas-Oisk (Izykh) ophiolitic belt that extends along the southern
margin of the terrane for over 500 km and consists of a melange zone
with ultramafic rock, gabbro, basalt and tuff, graywacke, chert,
siliceous shale, shale, and limestone. These oceanic crust rocks
comprise the basement of an island arc. (2) Volcanic island arc rocks
with magmatic arc, fore-arc, and back-arc basin facies. The basal part
of the magmatic arc consists of basalt-andesite-rhyolite and graywacke,
jasper, and chert. The volcanic rocks consist of bimodal units and local
boninitic dikes. The upper part of the magmatic arc consists of
differentiated, calc-alkaline, basalt-andesite-dacite-rhyolite with
thick tuff and coarse-clastic rocks, and reef limestone with Early
Cambrian archaeocyata and trilobites. Local limestone bodies occur in
olistostrome-like horizons. (3) Forearc basin trough units occurring in
the western part of the terrane (Arbat series and analogues) consist
mainly of turbidite with dominating shale and siltstone in a lower part,
and sandstone and siltstone in the upper part, with less abundant
volcanogenic, siliceous, and carbonate rocks with Early Cambrian
archaeocyata and Middle Cambrian trilobites in the upper part.
Olistostrome-like horizons with limestone olistoliths are common. And
(4) back-arc basin units occur in the eastern part and consist of
volcanomictic sand-silt-clay sedimentary rocks and lesser limestone,
coal shale, hematite-bearing jasperoid, basalt, rhyolite, and
conglomerate (Kolpin suite). The limestone contains Early Cambrian
archaeocyata and trilobites. The carbonate rocks define the flanks and
inner uplifts of a marginal sea (Balakhtison suite). Terrane is intruded
by Early Cambrian tholeiitic plagiogranite in the magmatic arc core, and
Ti- and Pt-bearing layered gabbro that formed in back-arc areas(?). The
eastern part of the terrane is intruded Middle Cambrian through Early
Ordovician(?) granitic batholiths of the collisional Tonnuola belt and
Early Devonian granitoids of the rift-related South Siberian belt.

**REFERENCES**: Zonenshain, 1963; Berzin, 1979; Berzin, Kheraskov, 1979;
Simonov and others, 1994; Kungurtsev, 1996.

## OD Olokit-Delunuran terrane (Accretionary wedge, type A) (Paleoproterozoic through Neoproterozoic) (Transbaikalia)

## 

Consists of two fragments, the Olokit and Delunuran fragments that are
separated by the Baikal-Muya island arc terrane. The Olokit fragment
forms a narrow band trending from the southwest (Lake Baikal area) to
the northeast (Vitim River area), and consists of small pre-Riphean
blocks of gneissic granite, Riphean shale and basalt, and melange lenses
of alpine-type ultramafic rocks. A U-Pb zircon isotopic age of the
gneissic granite is 2,040 to 1,700 Ma. The shale and basalt sequence
(Tyisky suite) occurs in narrow bands and wedges, and the basalt is
N-MORB and E-MORB type with a Sm-Nd whole-rock isochron age of 1050 Ma.
The Tyisky suite is concordantly overlain by a carbonaceous-sandy shale
sequence with polymetallic and iron quartzite ore bodies (Avkitsky
Suite). The sedimentary rocks in these suites are regionally
metamorphosed from greenscist facies to amphibolite facies,
kyanite-sillimanite subfacies. The Olokit fragment is deformed into
northeast-striking linear steep folds.

The Delunuran fragment occurs between the North-Asian Craton and the
Baikal-Muya terrane, and consists of Riphean metamorphosed sedimentary
rocks consisting, from bottom to top of: gneiss and schist (Danninsky
Suite); schist and calcareous rocks (Ust-Uriakh and Watershed Suites);
and schistose siltstone (Rodionovsky Suite). These units are regionally
metamorphosed to greenschist and amphibolite facies with assemblages of
staurolite-biotite-kyanite-muscovite, and
garnet-kyanite-biotite-muscovite (epidote-amphibolite and amphibolite
facies of kyanite-sillimanite type). The Delunuran fragment is deformed
into northwest-striking folds.

In the Olokit fragment, the Synnyrsky basin forms a major accretionary
structure and is 150 km long, and varies from 12 to15 km wide. The basin
contains: (1) a lower subaerial unit of variegated basalt, picrobasalt,
and tuff (Synyrsky suite); (2) shallow-water shaly sandy calcareous
dolomite (Protivo-Davan suite); and (3) conglomerate, shale, and
silty-sandstone (Avgolsky suite) that contain Late Riphean
stromatolites, microphytolites and micro-fossils; and (4) marine basalt,
siltstone, and hyaloclastic sedimentary rocks. The basalt exhibits a
Rb-Sr isotopic age of 670 Ma. The coeval Dovyren
dunite-troctolite-gabbrointrusive massif exhibits a Rb-Sr and Sm-Nd
isotopic ages from 740 to 700 Ma. The sedimentary rocks of the Synnyrsky
basin are deformed into inclined folds striking northeast to
north-south, monoclines dipping gently, or bedding that dips gently to
horizontally. Vendian overlap assemblage units, formed along a passive
margin, are terrigenous sedimentary rocks (Kholodninsky suite) in the
Upper Angara sedimentary basin. Terrane is intruded by late Paleozoic
intrusion of granite batholiths (Mama complex) with a U-Pb zircon age of
354 Ma, and by a syenite massif (Synnyrsky complex) with Rb-Sr whole
rock isotopic ages of 287 and 292 Ma. Accretion of the terrane to the
North-Asian Craton is interpreted as occurring in the Late Riphean.

**REFERENCES**: Tugarinov and others, 1976; Manuilova, Zarubin, 1981;
Bolonev and others, 1983; Bulgatov, 1983; Buldygerov and others, 1988;
Kislov and others, 1989; Dolnik and others, 1990; Neimark and others,
1990; Konnikov and others, 1994; Andreev and others, 1991; Pokrovsky and
Zhidkov, 1993; Rytsk and Shalaev, 1998.

## OG Ogcheon terrane (Accretionary wedge, type B) (Proterozoic) (Korea)

## 

Consists of pelitic, psammitic, calcareous sedimentary rocks, and mafic
rocks of the early Paleozoic Ogcheon Group, with pelitic rocks being
dominant. Also occurring are sparse pammitic rocks that are intercalated
with pelite, quartzite, metafeldspathic sandstone, and pepple-bearing
phyllite, along with local calcareous sedimentary and mafic rocks.
Metamorphism ranges from greenshist through transitional
greenshist-amphibolite to amphibolite facies. Shale with pebbles and
blocks of terrigenous, carbonate, and rarely chert are dominate.
Carbonate rocks contain an early Paleozoic fauna. The late Paleozoic and
early Mesozoic sedimentary rocks of the Pyeongnang Group contain
numerous granitoid and metamorphic rocks fragment. The Ogcheon Group is
probably a late Paleozoic and early Mesozoic olistrostrome formed in a
subduction zone. Metamorphism occurred during intrusion of Late
Permian-Triassic and Jurassic granite. Younger, northeast-striking
overlap pull-apart basins consist of epicontinental terrigenous deposits
of the Sindong and Hayan Groups and are interpreted as forming along an
Early Cretaceous transform margin. In the Late Cretaceous, volcanic
rocks of the Yuchon Group and the Bulgugsa granite intrusion are
interpreted as forming in a continental margin arc.

**REFERENCES**: Geology of Korea, 1993.

## OH Okhotsk terrane (Cratonal) (Archean through Jurassic) (Yakutia)

## 

Occurs adjacent to the southern termination of the North Asian Craton
Margin (Verkhoyansk foldbelt), and in ascending order consists of a
long-lived succession of units: (1) large blocks of Archean to
Paleoproterozoic gneiss and schist with a U-Pb zircon age of 3.7 Ga; (2)
gently-dipping, shallow-marine Middle and Neoproterozoic clastic and
carbonate rocks; (3) Early Cambrian limestone, marl, and sandstone; (4)
Early Ordovician conglomerate, limestone, marl, and sandstone with
macrofossils; (5) unconformably overlying Middle Devonian limestone,
sandstone, shale, and conglomerate, and Late Devonian rhyolite,
ignimbrite, andesite, dacite, and tuff that are interlayered with
nonmarine sandstone, siltstone, and conglomerate; and (6) mainly
nonmarine, rarely marine, clastic rocks of Carboniferous, Permian, Late
Triassic, and Early and Late Jurassic age. The ages are determined by
rare macrofossils and flora. Terrane contains local facies changes and
stratigraphic gaps, and unconformities occur at the base of the Late
Triassic and the Late Jurassic units.

Paleomagnetic determinations, moderate-quality data from Precambrian
(Riphean) sedimentary rocks and stromatolitic limestone yields a
southerly displacement with respect to the Siberian platform of
41^o^[+]{.underline}6^o^. The Okhotsk terrane is mostly overlapped by
Neocomian and Albian to Late Cretaceous nonmarine volcanic rocks of the
Uda volcanic-plutonic belt, and the Okhotsk-Chukotka volcanic-plutonic
belt. The Okhotsk terrane is correlated with the Omolon terrane of the
Kolyma-Omolon superterrane of the Russian Northeast, and with the
Kilbuck-Idono terrane of Alaska.

**REFERENCES**: Korol'kov and others, 1974; Vel\'dyaksov and Umitbaev,
1976; Avchenko, 1977; Chikov, 1978; Verzkhovskaya and Krichevets, 1987;
Pavlov, 1993.

## OI Orhon-Ikatsky terrane (Continental margin arc) (Late Neoproterozoic through Silurian) (Mongolia, Transbaikalia)

## 

In Transbaikalia, terrane strikes north-northeast and has dimensions
about 650 by 170 km. The geology of the terrane is reconstructed from
scattered fragments in the Barguzin-Vitim granitoid batholith. Terrane
primarily composed of terrigenous-carbonate, carbonate and
sedimentary-volcanogenic formations of Vendian-Cambrian, and, to a
smaller extent, of Ordovician and Silurian age. Also includes highly
metamorphosed rocks (Garginsky Suite) that are an uplift of an early
Precambrian basement. The Vendian-Cambrian sedimentary rocks include
fossiliferous limestone and dolomite. In the lower of the carbonate
section (Kurminsky, Tilimsky, Orochensky suites) are Early Cambrian
archeaocyates, chyolites, spucules of sponges. The overlying carbonate
sequences with shale interbeds (Ikatskyt and Yakshibsky Suites, Panovsky
Series) contain Early and Middle Cambrian trilobites. Older
sedimentary-volcanogenic sedimentary rocks (Balbagarsky and Itantsinsky
Suites) occur in the southern part of terrane and consist of mafic and
intermediate volcanic rock, chert-carbonate, and siliceous shale. The
sedimentary rocks are intruded by mafic intrusions of the Atarkhansky
and Ikatsky Complexes. Also occurring are small lenticular bodies of
dunite and harzburgite that are commonly serpentinized. A larger area of
flyschoid and terrigenous-volcanogenic rocks with sparse fossils may
constitute a younger Ordovician through Devonian assemblage. The
youngest unit is a Devonian variegated molassoid sequence (Bogdarinsky
Suite). Terrane is intruded bvy granitoids of the Barguzin-Vitim
batholith.

**REFERENCES**: Belichenko, 1969, 1977; Osokin and others, 1989; Butov
1996.

In northern Mongolia, terrane occurs in the Hangay Upland and Basin
along the Orhon River. Terrane extends for 1200 km and ranges from 30-50
km wide. Consists of late Riphean Early Cambrian volcanic and
sedimentary rocks that are subdivided into two complexes: (1) a lower
greenschist complex (Darhad Formation) that consists of quartz-chlorite
and quartz-biotite schist with metabasalt and porphyritic volcanic rock,
and lesser quartzite and stromatolitic limestone lenses; and (2) an
upper carbonate and schist complex (Buuraltay and Uldzitgol Formations)
that consists of siliceous slate, carbonaceous schist, phyllite, and
dolomitic limestone with Vendian to Early Cambrian stromatolites and
microphytolites. Units are zonally contact metamorphosed to high
temperature amphibolite facies, and contain sparse ultramafic rock and
gabbro bodies that probably are part of an Early Cambrian layered
complex. Terrane stitched by Bayangol calc-alkalic granite complex with
K-Ar isotopic age of 520 Ma, and by Devonian and Permian volcanic and
plutonic rock.

**REFERENCES**: Geology of Mongolian People's Republic, 1973,
Tomurtogoo, 1997, Badarch and others, 1999; Badarch and Bor-ming Jahn,
2000.

## OL Oldoy terrane (Passive continental margin) (Silurian through Early Carboniferous) (Southern Russian Far East)

## 

From base to top consists chiefly of: (1) Silurian quartzose sandstone,
siltstone, conglomerate, and minor limestone and Early Devonian
siltstone, sandstone, and conglomerate (Bolsheneversk and Omutninsk
suites); (2) Middle Devonian (Eifelian) limestone, sandstone, and
siltstone (Imchansk suite); and (3) Middle to Late Devonian
(Givetian-Fransian) sandstone, siltstone, and limestone, Late Devonian
(Fransian-Famennian) siltstone, sandstone, and limestone, and Early
Carboniferous (Tournaisian-Visean) sandstone, siltstone, conglomerate,
and limestone (Tiparinsk, Teplovsk, and Oedoisk suites). The Devonian
deposits contain abundant macrofossils including brachiopods, corals,
and bryozoans. The Early Carboniferous brachiopods and bryozoans are
Boreal. Silurian deposits are locally metamorphosed to lower greenschist
facies. Middle Paleozoic deposits are intruded by granodiorite, granite,
and diorite with K-Ar isotopic ages of 204 to 257 Ma and Rb-Sr isotopic
age of 256±7.35 Ma. Unconformably overlying overlap assemblages are: (1)
the Jurassic and Early Cretaceous Bureya sedimentary basin that formed
after amalgamation of the Oldoi and Gonzha terranes; and (2) Early
Cretaceous intermediate and silicic volcanic rocks, flora-bearing
nonmarine clastic rocks, and coeval granite and granodiorite of the
Umlekan-Ogodzhin volcanic-plutonic belt that also overlaps the Oldoi,
Gonzha, Mamyn, and Turan terranes.

**REFERENCES**: Krasny, 1966, 1973; Shilo, 1982; Martynyuk and others,
1990. Krasnyi and others,1996.

## OM Ondum terrane (Island arc) (Late Neoproterozoic through Ordovician) (Southern Tuva)

## 

Consists of two units. (1) A differentiated andesite-dacite-rhyolite
unit with tuff, breccia-lava, and subvolcanic rocks (Ondum suite) of
possible Vendian-early Cambrian age. Dacite and rhyolite varieties are
prevalent with minor basalt, and spares chert, jasperoid, and sandy
limestone. (2) A volcanic-sedimentary unit composed of coarse-clastic
tuffaceous terrigenous rocks at the base and carbonate rocks at the top
(Ilchir suite). The carbonates contain Early Cambrian archaeocyata.
Terrane also contains Middle-Cambrian through Early Ordovician(?)
granite of the Tonnuola collisional belt; and smaller bodies of Early
Devonian subalkaline granitoids of the rift-related South Siberian belt.

**REFERENCES**: Zaikov, 1976; Bukharov, 1979, 1981.

## ON Olenek terrane (Greenschist) (Paleoproterozoic) (Yakutia)

## 

Consists of metasandstone, metasiltstone, metapelite, and metavolcanic
rocks (Aekit series) that consists of metamorphosed rhyolite and dacite
(at the base), and basalt, andesite-basalt, and tuff (at the top).
Metamorphic grade varies from prehnite-pumpellyite to greenschist
facies. Primary sedimentary structures, such as bedding, rhythm, and
ripples are locally well preserved. Terrane is deformed into linear
isoclinal folds with axial planes dipping steeply southwest, and is
intruded by siliceous and intermediate dikes, potassic granite stocks,
and gabbro, diorite and granodiorite plutons. Muscovite from granite
exhibits a K-Ar whole rock isotopic age of 2,000 to 1,950 Ma, and a
biotite isotopic age of 2,080 to 1,846 Ma. Terrane is exposed in Olenek
uplift and is overlain by flat-lying Riphean deposits of the Siberian
Platform.

**REFERENCES**: Vishnevskiy and Krasil'nikov, 1963; Shpount and others,
1979; Rosen and others, 1994.

## OS Ononsky terrane (Accretionary wedge, type B) (Neoproterozoic? or Silurian?) (Transbaikalia, Mongolia) 

## 

In Transbaikalia, terrane, that extends about 2000 km and has a maximum
width of 150 to 200 km, defines the Mongol-Okhotsk suture zone of
central Mongolia and eastern Transbaikalia. Consists of several major
units from oldest to youngest. (1) Volcanic-sedimentary sequences
(Kulindinsky and Ononsky suites) metamorphosed to greenschist,
blueschist, and locally to epidote subfacies of amphibolite facies. The
Kulindinsky suite contains large ophiolite fragments with tectonic
wedges of metabasalt, blocks of massive and layered metagabbro, lenses
and slabs of alpine type ultramafic rocks. The metabasalt is derived
from N-MORB, E-MORB and OIB basalt, and has a Sm-Nd isotope model age of
583 Ma for the basalt protolith (S. Dril, unpublished data, this
report.). Metasedimentary rocks are mostly derived turbidites with
lesser deep-water chert metamorphosed to micro-quartzite. The Ononsky
suite is mainly terrigenous metasedimentary rocks with metamafic rocks
rapidly decreases from bottom to top. The age may be either Late
Riphean, based on poorly preserved microfauna of in schist, or Silurian
on the basis of structural position. (2) Early and Middle Devonian
sedimentary rocks of the Chindantsky and Ust-Borzja suites consist
mainly of terrigenous sedimentary rocks, often of turbidite origin, OIB
type metavolcanic rocks, and minor limestone and chert. The age of
suites is defined from fauna remains (Rutshtein and Chaban, 1997). (3)
Discordantly overlapping Late Devonian and Early Carboniferous
sedimentary and volcanic rocks (Makarovsky and Zunshiveisnky suites)
contain dacite, rhyolite, and siliceous tuff. The sedimentary rocks
contain Carboniferous brachiopods, byozoans, and crinoids. The
sedimentary rocks consist of non-metamorphosed terrigenous rocks, mainly
turbidite (Chironsky series) with abundant brachiopods, bivalves,
gastropods, and bryozoans. And (4) the youngest unit consists of Late
Triassic terrigenous sedimentary rocks (Mogoituy series) with *Monotis.*

Overlap and stitching complexes are the Trans-Baikalian-Daxinganling
sedimentary-volcanic plutonic that consists of Middle Jurassic
continental clastic sedimentary rocks (Karbachinsky series), and Early
Cretaceous rift-related volcanic-sedimentary formations (Turginsky
suite), and Middle and Late Jurassic granite (Kukulbey, Konduysky and
Shakhtaminsky complexes). These units define a time of accretion of
terrane to the North Asian Craton as pre- Middle Jurassic. Thrust and
strike-slip fault displacements along the Mongol-Okhotsk fault during
accretion resulted in local greenschist facies metamorphism.

**REFERENCES**: Okuneva and Konditerov, 1964; Kotlyar and Popeko, 1974;
Dolganev, 1963; Neelov, Milkevich, 1979; Gusev and Peskov, 1993; Dril
and others, 1994; Popeko, 1996; Rutshtein and Chaban, 1997; Rutshtein,
1997; Zorin and others, 1998a, 1998b.

In northeastern Mongolia, terrane occurs in a narrow, up to 30-70 km
wide and 1250 km long belt along the boundary of the Hangay and Hentiy
Uplands, along the southern border of the Hentey Upland. Terrane
contains fragments of Hangay-Dauria terrane and forms a large duplex
structure with southwest vergence. Terrane separated from Argunsky
terrane by Middle Mongolian Tectonic Line. Terrane consists chiefly of:
(1) schist and ophiolite in the central part; and (2) volcanic-carbonate
slate and flysch units near the Onon, Jargalant, and Duch Rivers with
Permian to Early Triassic fossils. The volcanic-carbonate slate units
(Upper Onon Complex) in the Onon River basin consist of metabasalt,
siliceous slate, and limestone with problematic fossils, and quartzite
interbeds. Complex was, previously dated as PreCambrian to Early
Cambrian but may be correlative with similar, fossil-bearing Early to
Middle Devonian units in the Tukuring fragment of the Argunsky terrane.
Metamorphic complexes occur in western and central parts of terrane and
consist of a greenschist complex in the west and black shale to the
east. Greenschist complex contains sandstone and siltstone, and minor
mafic volcanic rock and quartzite that are probably correlative to Upper
Onon Complex. The black shale consists of interbedded black shale
(carbonaceous schist), quartz-chlorite-sericite schist and mudstone with
quatrzite beds, and deformed lenses jasper that may be an olistolith.
Local Late Permian radiolarian occur in the jasper. The possible
ophiolite complex occurs along the Adaatsag melange zone, and consists
of serpentinized ultramafic rock, pyroxenite, and gabbro, with a diabase
dike and sill swarm, and variolitic tholeiitic basalt with a backarc
basin geochemical signature. The ophiolite age may be middle Paleozoic.
The terrane contains imbricated fault slices, thrusts, and duplex
structures that are overturned to the north and northeast. Stitch
complex consists of Triassic to Jurassic granite.

**REFERENCES:** Geology of Mongolian People's Republic, v. 1, 1973,
Tectonics of Mongolian People's Republic, 1974, Tomurtogoo, 1989, 1997,
Badarch and others, 1999; Parfenov and others, 1999.

## OT Onot terrane (Granite-greenstone) (Middle Archean? or Paleoproterozoic?) (Eastern Sayan)

## 

Forms a wedge among blocks of Sharizhalgay terrane, extends for 100 km
long, and ranges up to 30 km wide. Basal part consists of plagiogneiss
and tonalite- trondhjemite granitoids with relices of biotite and
biotite-hornblende migmatitic plagiogneiss and amphibolite forming
includions in plagiogranite. Plagiogneiss derived from high-alumina
tonalite-trondhjemite, and amphibolite derived from tholeiite basalt.
Plagiogranite exhibits a U-zircon isotopic age of 3.25 Ga. Upper part of
terrane consists of metavolcanogenic and metasedimentary rocks, mainly
biotite and amphibole-biotite gneiss and amphibolite with layers of
talc-serpentinite, metagraywacke, marble, and quartzite (Kamchadal suite
and Sosnovo-Baits suite). Metasedimentary rocks are intruded by gabbros
of the Arbansky complex. Near the terrane margin are rapakivi-like
granitoids (Shumikhinsky complex) with a Rb-Sr isotopic age of
1.983±0.048 Ba. Terrane is overlapped by terrigenous Late Riphean
sedimentary rocks (Ushakovsky suite) of the North Asian Craton.

**REFERENCES**: Bibikova and others, 1981; Belichenko and others, 1988;
Nozhkin, 1997.

## OZ Orogen-Zalantun terrane (Metamorphic) (Proterozoic) (Mongolia, Northeastern China)

## 

Extends to the northeast and consists of: (1) Paleoproterozoic
biotite-amphibole-plagioclase-gneiss, hornblendite, quartz-schist,
marble, and mica-schist that are metamorphosed to lower amphibolite
facies; (2) Neoproterozoic sericite-chlorite-schist,
sericite-quartz-schist, marble, ferroan quarzite, plagioclase-gneiss,
and other lower greenschist facies metamorphic rocks. Ordovician marine
terrigenous rocks and limestone unconformably overlap the terrane.

**REFERENCES**: Dong Shenbao, 1986; Zhou Yuwen and others, 1993.

## PP Poputninsk terrane (Oceanic) (Mesoproterozoic and Neoproterozoic) (Yenisey Ridge)

Occurs in the central part of the Yenisey Ridge and overthrust to the
east onto the Central Angara terrane. Terrane extends for 150 km long
and ranges up to 10-15 km wide. Consists mainly of a mafic-ultramafic
rock complex. Locally along the basal contact are green
quartz-feldspar-actinolite schist derived from andesic-mafic tuff,
pyroxenit and gabbro on differentiated sills, diabase dike complexes,
siliceous rocks, picrite, and ophiolite-clastic conglomerate and
gritstone. The middle and upper parts consist of altered pillow-basalt
and greenschist derived from tuff and hyaloclastite with local basalt
pillows. Basalt is similar to island arc and margin sea tholeiite in
terms of oxide and trace-element geochemistry. Terrane overlapped by
Late Riphean terrigenous-carbonate sedimentary rocks, and intruded by
calc-alkaline granite of the Tataka-Ayakhta complex with a U-Pb zircon
age of 760 Ma.

**REFERENCES**: Kornev and others, 1998; Kheraskova, 1999.

## PR Predivinsk terrane (Island arc) (Late Neoproterozoic) (Yenisey Ridge)

## 

Occurs in the southwestern Yenisey Ridge along the right bank of the
Yenisey River, extends in a submeridional direction for 70 km and ranges
up to 20 km wide, and is thrusted onto the Yenisey amphibolite-gneiss
terrane to the west. Consists of the Late Riphean and Vendian
metavolcanogenic and metrasedimentary rocks. The metavolcanic rocks are
mainly calc-alkaline basalt, andesite-basalt, andesite, dacite, and
rhyolite metamorphosed to greenschist facies. From mafic to siliceous
rocks, Sr decreases, K, Rb, Ba, and Th increase, and concentration of
high-field-strength elements distinctly increases. These geochemical
features, the prevalence of Na over K, the content of
high-field-strength elements in basalt close to MORB, and increased Fe
indicates an island arc formation. Gabbroc and
gabbro-diorite-plagiogranite massifs are associated with the volcanic
rocks. Thrust plates of paleooceanic rocks, including serpentinized
harzburgite, gabbro, and near-MORB tholeiite basalt occur in the eastern
and central parts of the terrane. Metabasalt occurs in overturned,
northeast-striking folds, and is the most deformed unit in the terrane.
Ultramafic rocks form zones of serpentinite melange, and metasedimentary
rocks, mainly quartzite, schale, and tuffaceous sandstone are less
abundant than volcanic rocks. A U-Pb zircon isotopic age for
calc-alkaline metarhyolite is 637±5.7 Ma. The western terrane margin is
overlapped by Middle Jurassic sandstone and shale with coal layers.

**REFERENCES**: Zablotsky and others, 1987; Vernikovsky and others,
1999.

## QT Qinghe-Tsel terrane (Metamorphic) (Mesoproterozoic and Neoproterozoic) (Northwest China, Mongolia)

## 

In Northwest China, strikes east-west and consists of two parts: (1)
Mesoproterozoic migmatite, schist, amphibolite, and migmatite
intercalated with marble containing remains of ancient micro-plants and
alga. (2) Low-grade metamorphosed Paleoproterozoic fine-grained clastic
rocks, mainly sandstone, siltstone, and mudstone. Unconformably
overlapping are Ordovician, Silurian and Devonian sedimentary rocks.

**REFERENCES**: Bureau of Geology and Mineral Resources of Xinjiang
Uygur Aut. Reg.(Xinjiang GMRB), 1990; Chen Zefu, 1997.

In southwestern Mongolia, terrane occurs in three separate small blocks
that occur on the southern margin of the Mongolian Altai and
northwestern side of the Gobi Altai Ranges. Blocks occur along the
Bulgan and Transaltai fault systems. Consists of polymetamorphosed and
polydeformed tonalite gneiss, amphibolite, schist with relics of
granulite, syntectonic granodiorite, and granite withU-Pb zircon
isotopic ages of 370 and 385 Ma, respectively (Mitrofanov and others,
1981; Kozakov, 1986; Bibikova and others, 1992). The protolith age of
metamorphic rocks and granulite-amphibolite facies metamorphism is
uncertain. Kozakov (1986) obtained Pb-Pb zircon ages ranging from 250 to
1120 Ma and 2200 Ma from gneiss. Intruding the terrane are the Gashuun
Nuur mafic dike complex, with Sm-Nd isotopic ages of 320 and 321 Ma
(Baykova and others, 1994) and Permian granite. Terrane interpreted as a
displaced fragment of pre-Altaid continental crust, or fragments of
Gondwana, or an accretionary wedge that presumably contains an inverted
metamorphic complex.

**REFERENCES**: Kozakov, 1986, Mitrofanov, 1986, Coleman 1991, Bibikova
and others, 1993; Dobretsov and others, 1995.

## RA Rudny Altai terrane (Island arc) (Late Silurian through Early Carboniferous) (Rudny Altai Upland)

## 

Bounded by the Irtysh and Northeast strike-slip fault zones. Composed
chiefly of middle and late Paleozoic sedimentary and magmatic units
formed in varying geodynamic environments. Oldest units are pre-Emsian
greenschist that occur in two large anticlines (Alei, Sinyushin, Irtysh,
and Zyryanov areas) consist mainly of Late Silurian and Early Devonian
age carbonate, sandstone, and shale with local fauna. Older, early
Palozoic units may exist. Units are interpreted as forming in a
convergent-transform margin along the North Asian Craton.

Unconformably overlying are less metamorphosed sequences with marine
fault that occur in asymmetric brachiform folds that are complicated by
the shearing and large-scale faulting. The sequences consist of several
sequences of Emsian through Early Carboniferous shallow-water marine
sedimentary-volcanogenic rocks. (1) The lower sequence of Emsian
sedimentary rocks contain a pebbly basal conglomerate with abundant
granitic pebbles, Eifelian-Early Givetial volcanic-sedimentary rocks
with mainly bimodal calc-alkaline volcanic rocks with subordinate
basalt, locally with pyroclastic and tuffaceous terrigenous facies. The
volcanogenic rocks are interbedded with sedimentary rocks. These units
are interpreted as forming along active continental margin consisting of
a region of convergent-transform interaction between oceanic and
continental plates that was accompanied by magmatism. (2) The next
sequence consists of unconformably overlying Late Givetian-Late Devonian
island-arc bimodal volcanic rocks with significant basalt and tuff. The
volcanic rocks range from basalt to rhyolite with mainly andesite and
dacite. In the Late Givetian-Late Devonian volcanic rocks decreased
eastwards and volcanomictic deposits increased. These deposits are
interpreted as a back-arc marine basin. (3) The next sequence consists
of Tournaisian-Early Visean terrigenous and carbonate rock (Tarkhan,
Bukhtarma and Ulbin suites) and overlying Middle-Late Visean volcanic
and sedimentary rocks (Larikhin and Ramanikhin suites). Volcanic rocks
are mainly andesite and basalt porphyry and lesser dacite, rhyolite, and
tuff. These units mark the end of the island-arc. (4) The next sequence
is Middle-Late Carboniferous molasse (Maloulbin suite) that locally
overlies the Devonian and Early Carboniferous sequences and consists of
basal andstone and conglomerate succeeded by siltstone and shale with
coal beds with plant fossils, sparse basalt porpohyry, and mafic and
siliceous tuff. Coeval granodiorite-tonalite batholiths (Zmeinogorsk
complex) also occur. (5) The youngest sequence is unconformably
overlying Late Carboniferous-Early Permian continental volcanogenic
molasse and occur in a small area in the central part of the terrane.
The volcanic rocks vary from andesite through dacite to rhyolite and are
intruded by leucogranite and granosyenite (Leninogorsk complex) with
isotopic ages of 277 to 266 Ma.

**REFERENCES**: Nekhoroshev, 1958; Kuzebny, 1975; Rotarash and others,
1982; Zonenshain and others, 1990; Dubatolov, 1994; Yolkin and others,
1994; Kozlov, 1995; Berzin and Kungurtsev, 1996.

## SA Sangilen terrane (Passive continental margin) (Paleoproterozoic or Neoproterozoic) (Southeastern Tuva, Mongolia)

## 

In northern Mongolia, consists of lower Proterozoic(?) marble,
amphibolite, schist, orthogneiss, and metapelite intruded by Ordovician
granodiorite and granite and Devonnian subalkalic granite. Overlain by
Permian non-marine subalkalic volcanic rocks and volcaniclastic rocks.
The Han Huhey block, that occurs on the southwestern margin of terrane,
east of Agardag fault, consists of (1) Archean gneiss and migmatite with
granulite inclusions; (2) Paleoproterozoic graphite marble and
quartzite; (3) Riphean metasandstone and dolomite intruded by lower
Paleozoic granite, granodiorite, diorite, and adamellite, and by
Devonian and Permian subalkalic and alkalic granitic rocks. Terrane is
interpreted to be a passive margin terrane, formed along the Sangelin?
cratonic block.

**REFERENCES**: Mitrofanov and others, 1981; Kozakov, 1986; Fedrovskii
and others, 1995.

In the Southern Tuva region, terrane consists of the Sizim, North
Sangilen, and South Sangilen blocks that are separated by sinistral
strike-slip faults that were later transformed into north-south-trending
thrust systems. Terrane consists of two thick, lithologic-petrographic
series, the lower Mugur-Teskhem gneiss-schist series, and the upper
Sangilen metaterrigenous-carbonate series. The Mugur-Teskhem
gneiss-schist series occurs mainly in the western South Sangilen block
and consists of gneiss and schist, and lesser marble, quarztite,
iron-bearing quartzite, and black shale that are metamorphosed to
amphibolite facies. The Sangilen series forms the most of the terrane,
occurs in all blocks, and consists of graphite-bearing marble,
marble-like limestone, quartzite, metamorphosed sandstone and shale that
are about 5000 m thick. The contact between these two series is unclear,
and is usually a thrust fault. The Sangilen series is interpreted as
Late Riphean, and may be stratigraphically overlain by
terrigenous-carbonate deposits with Early Cambrian archaeocyata. The
Mugur-Teskhem and Sangilen series comprise a thick terrigenous-carbonate
section interpreted as a Late Riphean passive margin of the North Asian
Craton. U-Pb isotopic data for metamorphic rocks of the Mugur-Teskhem
series show that the series is younger than 1130 Ma, regional
metamorphism occurred at about 1100 Ma, and high-temperature zonal
metamorphism occurred at about 440 Ma. The Sangilen terrane is locally
intruded by possible Cambrian and Ordovician granitic plutons that
probably occurred during strong deformation of the margin of the North
Asian Craton, during transform interaction of lithospheric plates. The
youngest plutons are of Early Devonian, within-plate plutons of
subalkaline granite, and small stocks of late Paleozoic-early Mesozoic
rare-metal granite.

**REFERENCES**: Alexandrov and others, 1981; Terleev and others, 1988;
Gibsher and Terleev, 1989, 1992; Il'in, 1982; Lebedev and others, 1991,
1993; Berzin and Dobretsov, 1994.

## SAL Salair terrane (Island arc) (Early Cambrian through Early Ordovician) (Salair Ridge)

## 

Consists of three large units. (1) An island-arc volcanic-sedimentary
sequence with Early Cambrian-Tremadoc marine fauna fossils. Sedimentary
rocks are limestone, sandstone, shale, siliceous shale, and
coarse-clastic rocks. Carbonate rocks are mostly Early Cambrian
(Gavrilov suite and analogurd) that range up to 2000 m thick, and the
latest Cambrian and Early Ordovician (Tolstochikhin suite and analogues)
that range up to 350 m thick. Several unconformities occur, a strong
deformation obviously occurred in the early Middle Cambrian with
deposition of molasse including conglomerate with granitic pebbles and
boulders (Bachat suite). (2) An island-arc sequence of localy magmatic
rocks that decreases upward. Rhyolite, andesite, basalt, and tuff occur
in the lower part of the section in the early Early Cambrian(Ancheshev
suite), and basalt and andesite (Pryamushin, Bachat, and Orlinogor
suites) occur in the late Early Cambrian. The Middle Cambrian-Early
Ordovician units contain sparse to no volcanic rocks, and decrease.
Southward. And (3) a sedimentary-volcanic sequence consists of
subvolcanaic plaigogranite, plagiogranite-porphyry, diabase and small
intrusions of diorite, gabbro-diorite and gabbro. Up section, these
rocks exhibit low and moderate alkalinity, increasing K content,
increasing Na and lowering Ti.

Overlap assemblage rocks consist mainly of Ordovician, Silurian, Early
Devonian, and Eifelian shallow-marine carbonate-terrigenous
moSouthlasse. In the southwestern part, the terrane is conformably
overlain by carbonate-terrigenous rocks. From east to west, the
shallow-water sedimentary rocks are replaced by deeper units in the
Ordovician, Silurian and Early Devonian. Deeper marine deposits formed
in the Late Devonian and Early Carboniferous after a Late Givetian
pause. No essential re-structuring has been fixed. Terrane is intruded
by small bodies of late Paleozoic-early Mesozoic, within-plate
granitoids.

The Salair terrane was structurally imbricated in the late Paleozoic and
early Mesozoic, and thrust over the continental Carboniferous-Permian
deposits of the Kuznetsk basin to the east. The northwest Salair terrane
is underthrust the Late Devonian and Early Carboniferous marine
sedimentary strata of the Kolyvan-Tomsk marine basin.

**REFERENCES**: Resolutions, 1979; Grigor\'yev, 1988; Yolkin and others,
1994; Tokarev and others, 1996.

## SE Seluohe terrane (Accretionary wedge, type B) (Neoproterozoic) (Northeastern China)

## 

Occurs at the northern margin of the Archean Jilin-Liaoning-East
Shandong terrane of Sino-Korean Craton. Consists of the Neoproterozoic
Seluohe group composed of metamorphic rocks. The lower member of the
Seluohe Group consists of metamorphosed basalt and andesite tuff and
intercalated metamorphosed rhyolitic tuff and local dolomitic marble.
The upper member of the Seluohe Group consists of felsic lava and
intercalated granulite, biotite-chlorite schist, and amphibolite.
Several volcanic eruptive cycles are recognized. Terrane generally
exhibits greenschist facies metamorphism. However, recent studies
indicate the Seluohe group consists of tectonic sheets of various
origins and metamorphic grades and may constitute a melange.

**REFERENCES**: Bureau of Geology and Mineral Resources of Jilin
Province, 1989; Krashyi and others, 1996; Lu Jiansheng and others, 1996.

## SG Sergeevka terrane (Island arc) (Cambrian? and Ordovician?) (Southern Russian Far East)

## 

Consists chiefly of a long-lived and complex terrane composed of two
major units: (1) An older unit of syntectonic, migmatitic, gneissic
gabbro and quartz diorite that contain xenoliths up to several hundred
meters in size. The xenoliths are composed of amphibolite, quartzite,
marble, and calc-schist. The gneissic structure in the gabbro and
diorite parallels the schistosity in the xenoliths. The amphibolite
xenoliths are derived from oceanic tholeiite whereas the gneissic gabbro
and quartz diorite are derived from a continental-margin arc. U-Pb
zircon isotopic analyses exhibit intrusive ages of about 500 to 527 Ma.
And (2) a younger unit of the Early Ordovician biotite-muscovite Taphuin
Granite with a Ar-Ar muscovite isotopic age of 491 Ma. The granite forms
a major thrust overlying gneissic gabbro and associated rocks.

Overlapping units are: (1) Unconformably overlhing Middle and Late
Devonian felsic tuff, conglomerate, and sandstone with flora; (2)
conformably overlying Early Carboniferous nonmarine conglomerate,
flora-bearing sandstone, and felsic tuff; (3) Permian conglomerate,
sandstone, mudstone, basalt, andesite, rhyolite, and reef-forming
limestone; (4) Late Permian olistostromes; (5) unconformably overlying
Middle Triassic to Middle Jurassic shallow-marine marine sandstone and
siltstone; and (6) conformably overlying Middle and Late Jurassic,
subduction-related(?) rhyolite, andesite, and basalt to the south, and
Late Jurassic, extension-related basalt and picrite to the north; and
(7) Cretaceous and younger terrestrial coal-bearing deposits. The
Sergeevka terrane was amalgamated with other terranes of the Khanka
superterrane during the early Paleozoic, and in the Early Cretaceous,
the Khanka superterrane was accreted to the eastern margin of Asia. The
Late Cretaceous and Paleogene calc-alkalic volcanic rocks of the East
Sikhote-Alin volcanic-plutonic belt (unit es) overlap all terranes of
the Sikhote-Alin region.

**REFERENCES**: Krasny, 1966, 1973, Bersenev, 1969, Shilo, 1982;
Nazarenko and Bazhanov, 1986; Khanchuk and others, 1988; Sinitsa and
Khanchuk, 1991; Natal'in, 1991, 1993; Khanchuk, 1993; Aleinikoff and
others, in press.

## SH Shalaurov terrane (Accretionary wedge, type B) (Permian and Triassic) (Yakutia)

## 

Occurs on southeast Bolshoy Lyakhov Island and consists serpentinized
peridotite, MORB-type pillow basalt with a Sm-Nd isotopic age of 291+62
Ma, and amphibolite with a K-Ar isotopic age of 473 Ma. Units comprise a
tectonic sheet that is thrust over the Permian and Triassic flysch to
the north that are intruded by granite with K-Ar ages of 100 to 110 Ma.
Permian and Triassic rocks terrane may be northernmost fragment of the
Kular-Nera slate belt described above.

**REFERENCES**: Parfenov, 1984; Drachev and Savostin, 1993; Nokleberg
and others, 1994.

## SHA Sharizhalgay terrane (Tonalite-trondhjemite gneiss) (Archean through Paleoproterozoic) (Transbaikalia, Eastern Sayan)

Occurs to west of Lake Baikal, extends more than 300 km long and ranges
up to 50 km wide, and consists of several large blocks comprising an
uplifted basement of the Siberian Platform composed of early Precambrian
(Archean and Paleoproterozoic?) granulite-gneiss complexes. Terrane
consists of: (1) Erminsky Suite consisting of biotite and
biotite-hornblende gneiss, schist, and amphibolite; (2) Shumikhinsky
Suite consisting of diopside- and hypersthene-hornblende schist and
amphibolite; (3) Zhidoysky Suite consisting of biotite-hypersthene,
biotite-two-pyroxene gneiss and granulite with interlayered pyroxene,
pyroxene-hornblende schist; and (4) Zaginsky Suite consisting of
biotite, biotite-pyroxene plagiogneiss, two-pyroxene schist, and
ferruginous quartzite. units are metamorphosed to granulite facies. The
Kitoy Suite (Sharyzhalgay Series), that differs from underlying suites
in composition, type of folding, and metamorphism, contains
high-aluminous sillimanite schist, amphibole, garnet-pyroxene-amphibole
plagiogneiss with lenses of garnet-biotite and garnet-sillimanite
plagiogneiss, marble, and calciphyres. Recent U-Pb, Rb-Sr and Sm-Nd
isotopic ages for the Sharyzhalgay Series are 2.42-2.27 Ga (age of
protolith for granulite and charnokite), and 1.9-1.8 Ga (age
metamorphism and migmatisation). Terrane is overlapped by the Riphean
and Paleozoic sedimentary cover of the North Asian Craton.

**REFERENCES**: Volobuev and others, 1980; Bibikova and others, 1981;
Petrova, Levitsky, 1984; Belichenko and others, 1988; Sklyarov and
others, 1998; Aftalion and others, 1991.

## SHE Shevli terrane (Passive continental margin) (Early Cambrian through Late Devonian) (Northern part of Russian Southeast)

Consists of following deposits from bottom to top: (1) Early Cambriam
units, with Sibirian-affinity archeocyats, including Tokhikan suite (red
conglomerate, sandstone, siltstone, limestone, and sparese basalt,
andesite, and tuff), Malotokhikan suite (basalt, andesite, and sparse
conglomerate, sandstone, and limestone), Ust-Tipton suite (sandstone,
siltstone, conglomerate, and limestone), and Shevli suite (limestone,
dolomite, and marl). Early Cambrian ones; (2) Late Cambrian Rybalka
suite (limestone and marl with sandstone and siltstone interbeds); (3)
Early Ordovician Ust-Bugali suite (sandstone, siltstone, conglomerate,
and limestone); (4) Late Devonian sandstone, and siltstone. Overlapping
sedimentary and volcanic assemblages are: (1) Jurassic shallow-marine
deposits (Uda sedimentary basin); and (2) Early Cretaceous non-marine
clastic deposits (Bokon suite) including andesite and tuff.

**REFERENCES**: Kirillova and Turbin, 1979; Popeko and others, 1993;
Krasni and others, 1996.

## SHK Sangun-Hidagaien-Kurosegawa terrane (Island arc) (Silurian through Permian) (Japan)

## 

Consists mainly of various tectonic blocks of low- to
intermediate-pressure type metamorphic rocks with Rb-Sr whole-rock
isotopic ages of 350 to 400 Ma, Ordovician ophiolite with local highly
sheared serpentine matrix, Ordovician through Permian sedimentary rocks,
and Mesozoic sedimentary rocks. The middle Ordovician to Devonian
sedimentary rocks consist of melange and turbidite, mainly shale and
siliceous tuff that are partly metamorphosed to high P/T conditions. The
Carboniferous and Permian rocks consist of shallow-marine continental
shelf deposits, mainly shale, sandstone, conglomerate and limestone,
with a large amounts of Carboniferous pyroclastic rocks.

**REFERENCES**: Suzuki and others, 1979; Igo, 1990; Nishimura
1990;Yoshikura and others, 1990, Tazawa, 2000.

## SHM Shimanto terrane (Accretionarry wedge, type A) (Early Cretaceous through Miocene) (Japan)

## 

Consists mainly of thick coarse-grained flysch tectonically intercalated
thin melange zones that occur along north-dipping thrust faults with a
reconstructed ocean-plate stratigraphy for melange zone. Minor basaltic
rock and chert occur along with predominant clastic rocks. Melange units
form thin tectonic slivers in thick, coherent turbidite units. Melange
contains varicolored shale, radiolarian chert, red shale, pillow basalt
lava, and nannoplankton limestone that all occur in a random manner.
Melange was highly sheared during tectonic mixing. Terrane contains four
subterranes, from north to south, a Early to mid-Cretaceous, a Late
Cretaceous, Eocene, and early Miocene subterranes. The thickness of the
Late Cretaceous (Shimanto) subterrane ranges from 500 m to 1,500 m.
Terrane contains tight isoclinal folds. Thickness of Tertiary
subterranes ranges from 1,000 m to 2,000 m. The rate of convergence
ranges from 4 to 6 cm per year. The age of subducting oceanic plate is
younger than 10 Ma. Terrane is separated from the Jurassic accretionary
complex to the north by a major thrust fault, the Butsuzo tectonic line.

**REFERENCES**: Taira, 1981, 1988.

## SHT Shmidt terrane (Island arc) (Late Jurassic through Late Cretaceous) (Southern Russian Far East)

## 

From oldest to youngest, consists chiefly of three units. (1)
Serpentinite melange that consists of harzburgite, cumulate gabbro,
high-Ti dikes, basalt, and Late Jurassic to Early Cretaceous radiolarian
chert (Tominskia sequence) that is interpreted as a subduction zone
complex. (2) Bimodal sheeted dikes and flows and siliceous tuff with
mid-Cretaceous (Albian to Cenomanian) radiolarians, and plagiogranite.
The bimodal igneous rocks are geochemically similar to primitive island
arcs. And (3) an upper unit of basalt, andesite, tuff, argillite, and
sandstone with Cenomanian to Santonian *Inoceramus* (Slavyansk
sequence).

**REFERENCES**: Geology of the U.S.S.R., Sakhalin Island, 1970;
Raznitsin, 1982; Yurkova, 1991.

## SHU Shutkhulai terrane (Metamorphic) (Late Neoproterozoic) (Eastern Sayan)

## 

Occurs in a large lens along the margin of the Tuva-Mongolian
superterrane, chiefly consists of mica schist, schist and marble
metamorphosed to amphibolite facies, and minor metavolcanic rocks. Age
unknown but infered as Late Neoproterozoic. Terrane interpreted as a
small fragment of the Riphean passive-continental margin of the North
Asian Craton. Structural position is similar to that of the Derba and
Sangilen terranes. Terrane intruded by early and middle Paleozoic
granitoids of the Tannuola and South Siberian belts.

**REFERENCES**: Makhin, 1959; Kudryavtsev, 1960; Altukhov, 1986;
Polkanov and Obruchev, 1964; Il'in and Parfenov, 1967.

## SK South Kitakami terrane (Island arc) (Silurian through Permian?) (Japan)

## 

Consists mainly of Paleozoic to Mesozoic sequences including ophiolite,
metamorphic rocks, and granite of early Paleozoic age. Units include
clastic and carbonate rocks, calc-alkalic rhyolite to dacite volcanic
rocks, and the early Paleozoic Hikami Granite. Oldest layered rocks
contain Silurian fossils. Terrane overlain by Triassic, Jurassic and
Early Cretaceous shallow-marine clastic sedimentary rocks and lesser
volcanic rocks, unconformably overlapped by Late Cretaceous rhyolite,
and intruded by Late Cretaceous Granite.

**REFERENCES**: Mori and others, 1992.

## SL Solon terrane (Accretionary wedge, type B) (Late Carboniferous through Permian) (Northeastern China, Mongolia)

## 

In Chna, occurs on the north of the Solon-Xarmolonhe fault, strikes
east-west, and composed mainly of two units: (1) Middle and Late
Carboniferous ophiolite, limestone, and chert containing foraminifera,
fusulinida, polyp coral, brachiopods, and other marine fossil; (2) a
Carboniferous subduction-related ultramafic plutonic mass; and (3)
Permian volcanoclastic rocks, andesite, tuffaceous sandstone, and
sandstone and conglomerate with brachiopods. Overlapping units are
Jurassic volcanoclastic and sedimentary rocks. Terrane is interpreted as
forming during subduction of late Paleozoic ocean crust.

**REFERENCES**: Xie Tonglun, 1980; Cao Congzhou, 1987; Bureau of Geology
and Mineral Resources of Inner Mongolian Aut.Reg. (Inner Mongolian
GMRB), 1991; Wang Ying, 1991.

In southeastern Mongolia occurs south of the Hutag Uul terrane near the
China-Mongolia border. Consists of a structurally complex assemblage of:
(1) dismembered Solon ophiolite of presumably Upper Devonian to Lower
Carboniferous age; (2) Early Carboniferous sandstone, siltstone and
limestone, minor conglomerate; (3) Middle Carboniferous to Early Permian
fusulinid-bearing massive limestone, minor conglomerate, and sandstone;
(4) Late Carboniferous to Early Permian andesite, dacite, tuff,
sandstone, and siltstone, and minor fossiliferous limestone; (5) Late
Carboniferous to Early Permian tholeiite pillow basalt, basaltic
andesite, chert, tuffaceous sandstone, and siltstone containing
olistostrome; and (6) Late Permian conglomerate, sandstone, siltstone,
and chert. Terrane also contains undated greenschist to amphiboite
facies metamorphic rock that is intruded by gabbro and granodiorite.
Terrane overlain by Early Cretaceous conglomerate, sandstone, and
volcanic rock, and is intruded by Triassic plutons .Tterrane is
interpreted as an accretionary wedge with fragments of island arc,
back-arc, and forearc basin sedimentary rock, seamount volcanic rock,
and associated rock.

**REFERENCES**: Tectonics of Mongolian People's Republic, 1974;
Ruzhentsev and others, 1989; Pavlova and others, 1991.

## SM Sisim terrane (Island arc) (Cambrian) (Eastern Sayan)

## 

Consists of two units. (1). Early Cambrian metamorphosed basalt,
keratophyre, volcaniclastic rocks, and sparse lenses of limestone
(Kolpin suite); and (2) an unconformably overlying carbonate-tuffaceous
terrigenous unit with a lower part composed of massive and platy
limestone and basal conglomerate (Lodochnaya suite), and an upper part
composed of interlayered tuff, tuffaceous sandstone, tuffaceous
conglomerate, siltstone, and mudstone (Katel suite). Both units contain
Middle Cambrian trilobites (Amgaian). Terrane also contains Cambrian,
Ordovician and Silurian(?) collisional granite (Tannuola belt) and Early
Devonian subalkaline granite of rift-related South Siberian
volcanic-plutonic belt. Terrane unconformably overlapped by a Early
Devonian sedimentary-volcanogenic complex that grades upward into Middle
Devonian and Carboniferous continental molasse.

**REFERENCES**: Musatov, Nemirovskaya, 1961; Predtechensky, 1967;
Amgaian, 1971.

## SMA Samarkina terrane (Accretionary wedge, type B) (Late Permian through Middle Jurassic) (Southern Russian Far East)

## 

Occurs along eastern edge of the Khanka-Bureya superterrane and extends
northeast from southern coast of Primorye to Amur River, and ranges up
to 100 km wide. Consists of rocks that vary widely in lithology, age,
and genesis, including: (1) continental-margin deposits (turbidite and
accretionary melange), pelagic chert, and siliceous mudstone that occur
in various thrust panels and slices, variable-size lumps and blocks; and
(2) fragments of seanmounts including basalt, limestone, and ophiolites.
The marine formations occur in thrust slices up to 20 km long and range
from several tens up to several hundreds meters thick. Chert slices are
locally repeated three to five times. Large slices are usually underlain
by melange with lumps and blocks of the same units.

Terrane consist of a minimum of five successive tectono-stratigraphic
units that are subdivided into Sebuchar and Eldovaka subterranes. Each
unit composed of marine rocks that grade smoothly upward into
continental-margin terrigenous rocks grade into olistostromes in an
accretionary melange. Uppermost structural level is the Sebuchar
subterrane that contains accreted fragments of an oceanic plateau with
slices and blocks of: (1) middle Paleozoic gabbro-ultramafic rocks
(Kalinovka Formation); (2) basalt with overlying Late Devonian(?) and
Early Permian chert, Carboniferous and Permian limestone, and Permian
black mudstone (Sebuchar Formation); and (3) Late Permian greenish-grey
and green sandstone alternating same-colour siltstone (Udeka Formation).
The other four tectono-stratigraphic units are the Eldovaka subterrane
that forms the middle and lower structural levels of the Samarka
terrane. The subterrane consists of chert overlapped by turbidite
deposits (Eldovaka Formation) with local basalts underlying some chert
slices. Age of chert ranges from Late Permian thorugh Middle Jurassic,
whereas the age of turbidite and accretionary melange is Early to Late
Jurassic. The structure of the Samarka accretionary prism is a multiple
layered cake with relatively younger terrigenous deposits alternating
with older marine rocks. The relationship between various formations of
the Samarka prism in modern Sikhote-Alin structure are faults.
Unconformably overlying units are Valanginian clastic marine rocks and
unconformably overlying Albian clastic marine rocks.

**REFERENCES**: Khanchuk and others, 1988, Kemkin and Khanchuk, 1993a,
Kemkin and Philippov, 2000.

## SN Saratan terrane (Oceanic) (Late Neoproterozoic and Early Cambrian) (Eastern Gorny Altai)

## 

Consists of two presumably Vendian-Early Cambrian volcanic-sedimentary
units. (1) A lower unit (Saratan sequence) chiefly composed of mafic
volcanic rocks and tuff that are metamorphosed to
epidote-chlorite-actinolite schistm and interlayered metamorphosed
siliceous rocks and siliceous shale. The volcanic rocks are high-Ti
tholeiitic MORB and OIB types. (2) An upper unit (Karagol sequence),
formed in a back-arc island-arc environment, consists of locally
occurring basal conglomerate, tuffaceous sedimentary rocks, and minor
volcanic rocks that range from basalt to plagiorhyolite. Sedimentary
rocks are sandy shale and lesser metachert and limestone. Also occurring
are small serpentinite and gabbro bodies; the serpentinite occurs mainly
within melange zones of tectonically imbricated units. Granitoids
consist of Devonian calc-alkaline and plumasitic granite, and late
Paleozoic and early Mesozoic subalkaline and alkaline granite.
Overlapping units are Early Devonian and local Early and Middle
Carboniferous volcanic-sedimentary rocks. The complicated outlines of
terrane are the result of imbricated-thrust and strike-slip faulting.
Local blueschist metamorphism with Na amphibole (crossite) and
glaucophane.

**REFERENCES**: Dergunov, 1967; Dong and others, 1985; Gusev, 1991;
Maruyama and others, 1996; Shokalsy and others, 1997; Vladimirov and
others, 1997.

## SP Spassk terrane (Accretionary wedge, type B) (Cambrian and older through Early Silurian) (Northeastern China, Southern Russian Far East)

## 

In northeastern China, consists chiefly of: (1) amphibolite derived from
mafic and ultramafic rocks, and calc-schist; and (2) Early Cambrian
slate, marble, phyllite, and gneiss containing *Archaeolynthus
sibiricus* and *Ajacicyathus sp*. Overlap assemblages are Late Permian
conglomerate, sandstone, phyllite, marble, slate, and tuff. Terrane is
possibly intruded by the Silurian, late Paleozoic, and Early Cretaceous
plutons.

**REFERENCES**: Bureau of Geology and Mineral Resources of Heilongjiang
1993; Nokleberg and others, 1994; Tang Kedowg and others, 1995; Khanchuk
others, 1996; Krasnyi and others, 1996; Sun Jiapeng and others, 2000.

In Russian Southeast, consists chiefly of four major units: (1) undated
turbidite and olistostrome deposits with Tommotian limestone fragments;
(2) limestone, with Atdabanian archaeocyathids, and interlayered chert
with a structural thickness of at least 3,000 m; (3) ophiolite-derived
ultramafic and mafic rocks, serpentinite melange, and basalt that are
overlapped by limestone and interlayered mudstone and that contain
Lenian archaeocyathids and trilobites, with a minimum structural
thickness of 1,700 m; and (4) conglomerate, sandstone, and siltstone
derived from units (2) and (3) with Early and Middle Cambrian trilobites
and brachiopods, and Ordovician and Early Silurian conglomerate. Terrane
intruded by postaccretion middle Paleozoic, Carboniferous, and Late
Permian granitic rocks, and overlain by Devonian, Mississippian, and
Permian volcanic and sedimentary rocks that constitute overlap
assemblages for the entire Khanka superterrane. Albian granitic rocks
are interpreted as forming in a continental margin, transform-margin
arc. The Late Cretaceous and Paleogene calc-alkalic volcanic rocks of
the East Sikhote-Alin volcanic-plutonic belt overlap the Spassk and all
other terranes of the southern Russian Far East.

**REFERENCES**: Shcheka and others, 1973; Nazarenk and Bazhanov, 1987;
Belyaeva, 1988; Natal'in, 1991, 1993; Khanchuk, 1993.

## SR Sarkhoy terrane (Island arc) (Late Neoproterozoic) (Northern Mongolia, Eastern Sayan)

## 

In northern Mongolia, forms a north-south trending belt west of Hovsgol
Lake, and consists of late Riphean basalt, andesite, dacite, rhyolite,
tuff, conglomerate, sandstone, siltstone, dolomite, and limestone.
Volcanic rocks are intruded by coeval riebeckite granite with a K-Ar
isotopic age of 752 Ma. A granite clast from conglomerate has a K-Ar
isotopic ages of 823 and 718 Ma. Volcanic rocks are interpreted as part
of a calc-alkaline island arc according to petrochemical and trace
element data (Konnikov and others, 1994). The terrane overlain by
Vendian to Early Cambrian sedimentary rock, Permian volcanic and
sedimentary units, and Jurassic molasse, and are intruded by Middle to
Late Cambrian, Devonian, and Permian granite.

**REFERENCES:** Il'in, 1973; Buyakite and others, 1989; Konnikov and
others, 1994; Byamba, 1996.

## SS Sosunay-Langeri terrane (Accretionary wedge, type B) (Jurassic through Paleogene) (Southern Russian Far East)

## 

Consists of the Susunay and Langeri metamorphic complexes. The Susunay
complex occurs in southern Sakhalin Island and consists of the packet of
tectonic nappes. The lower tectonic nappes mainly siliceous and volcanic
rocks and the upper nappes contain mainly terrigenous rocks. Units
contain Early Triassic through Early Cretaceous conodonts and
radiolarians. Volcanic rocks are tholeitic, subalkaline, and alkaline
basalt formed in abyssal plates or ocean islands. Overlying units are
interbedded siliceous and terrigenous rocks that grade upward into
flysch with interlayered tuff and sandstone with carbonate concretions
and that contain Late Cretaceous and Paleogene(?) radiolarians. Terrane
metamorphosed to greenschist facies with K-Ar metamorphic isotopic ages
of 60 to 55 Ma. The foots of tectonic nappes contain serpentinite
melange with blocks of ophiolite, eclogite with K-Ar isotopic age of
133Ma, amphibolite with K-Ar isotopic age of 206 and 178 Ma, and
glaucophane schist with K-Ar isotopic age of 90 to 95 Ma.

The latter Langeri metamorphic complex occurs in the western foothills
of the East Sakhalin Mountains and consists of nappe packets composed of
Jurassic and Early Cretaceous volcanic rocks with rare chert interbeds
and Late Cretaceous laminite metamorphosed from prehnite-pumpellyite up
to low-grade biotite greenschist facies with K-Ar ages of 71-58 Ma.
Metamorphism intensifies down structure. Local serpentinite melange in
the base of the tectonic nappe packet contains blocks of ultramafic
rocks, amphibolite, amphibole- and quartz-mica schist metamorphosed to
blueschist facies with K-Ar isotopic age of 92 Ma.

**REFERENCES**: Rikhter, 1986; Zinkevich and others, 1999.

## SU Sugash terrane (Island arc) (Early and Middle Cambrian) (Southern Gorny Altai)

## 

Forms a tectonic sheet in between Kaitanak oceanic terrane and Altai
continental-margin turbidite terrane and consists of clastic rocks and
basalt, minor plagiorhyolite, and small hypabyssal diorite and gabbro
bodies (Sugash suite). Basalt is mainly MORB or island-arc tholeiite
type. are present. The Early-Middle Cambrian age is inferred. Terrane is
intruded by Devonian granitoids of the Altai volcanic-plutonic belt.

**REFERENCES**: Shokalsky and others, 1997.

## SW Sambagawa terrane (Metamorphic) (Cretaceous) (Japan)

## 

Consists of greenstone, chert, and graphite metapelite. Sedimentary
rocks contain Carboniferous, late Triassic, and Late Jurassic
microfossils. Metamorphic grade range from high pressure type
epidote-amphibolite facies to greenschist facies. Metamorphic ages range
from 65 to 120 Ma.

REFERENCES: Miyashiro and Banno, 1958; Banno, 1964.

## TA Talitsk terrane (Continental-margin turbidite) (Cambrian through Early Triassic) (Northwestern Gorny Altai)

## 

Chiefly composed of: (1) Cambrian sandstone-siltstone flysch sequence
with coarse-clastic interbeds that occurs in windows inbetween plutons;
(2) small sheets and tectonic lenses of strongly imbricated
Ordovician-Silurian volcanic-siliceous rocks that occur the marginal
areas of the terrane; (3) Late Devonian calc-alkaline and plumasitic
granite; and (4) Late Permian and Early Triassic REE granite, and. The
sequence is correlative with the Charysh and Suetka suite of the Charysh
terrane, but unlike the Charysh terrane, contains the
Ordovician-Silurian units.

**REFERENCES:** Iwata and others, 1997; Shokalsky and others, 1997;
Vladimirov and others, 1997

## TB Tumangang terrane (Island Arc) (Late Carboniferous and Permian) (Korea)

## 

Consists of the Tuman Group that contains: (1) Late Carboniferous(?) and
Early Permian Amgi Formation composed of biotite-siliceous shale with
interlayered quartzite and limestone; (2) Early Permian Kyorensang
Formation composed of basalt and andesite lava and tuff, aleurolite,
shale, and limestone; and (3) Late Permian Songsang Formation composed
of aleurolite, shale with interlayered siliceous sandstone and volcanic
rocks. Terrane intruded by Late Permian granite (Tumangang Complex) and
the Jurrassic Daebu granite, and is overlapped by Tertiary
epicontinental deposits and volcanic rocks (Hamyon and Obong Groups).

**REFERENCES**: Geology of Korea, 1993.

## TD Tukuringra-Dzhagdy terrane (Accretionary wedge, type B) (Silurian through Permian) (Southern Russian Far East)

## 

Consists chiefly of following fault-bounded units: (1) tectonic lenses
or olistoliths of Neoproterozoic limestone with oncolite and
catagraphite; (2) Silurian and Devonian mafic volcanic rocks and chert
with lesser terrigenous rocks and limestone; (3) Late Carboniferous
sandstone, siltstone, shale, and turbidite (Dzheskogon and Nekter
suites); (4) Permian flysch, greenstone, chert, and limestone with
Tethyan corals and fusulinids (Bochagor suite); and (5) a narrow
tectonic lens of ophiolite (Pikansk complex) that occurs along southern
margin of terrane, and consists of gabbro, amphibolite, pyroxenite,
serpentinite, and plagiogranite. Sparse Early to Middle Devonian corals
and crinoids occur in the limestone; and Givetian brachiopods in the
siltstone. Late Permian Tethyan fusulinids that in the Bochagor suite
are paleobiogeographically distinct from those in adjacent terranes.
Terrane generally metamorphosed to schist and microquartzite at
greenschist facies. Relic glaucophane schist occurs in western part of
the terrane. Six stages of collisional deformation are recognized.
During the main, initial stage, north-verging, recumbent and overturned
isoclinal folds and thrusts formed. A penetrative ductile, stretching
lineation formed during subsequent strike-slip terrane transport. The
northern part of the terrane is overlain by Middle to Late Jurassic
continental terrigenous deposits; and the southern part is overlain by
Early Cretaceous Umlekan-Ogodzhin volcanic-plutonic belt. Terrane is
interpreted as tectonically linked to the Uda volcanic plutonic belt
that formed part of the Mongol-Okhotsk active continental margin along
the Stanovoi block of the North Asian Craton.

**REFERENCES**: Kirillova and Turbin, 1979; Natal'in and others, 1985;
Kozlovskiy, 1988; Natal'in, 1993; Krasni and others, 1996.

## TE Tersa terrane (Oceanic) (Late Neoproterozoic) (Central Kuznetsk Alatau, Altai)

## 

Consists of a package of tectonic sheets of back-arc units that gently
dip north-northeast and are composed of a tectonically imbricated
ophiolite melange. The ophiolite consists of a succession of dunite and
harzburgite, dunite and wehrlite and clinopyroxenite, layered gabbro and
ampohibolite, and mafic volcanic rocks metamorphosed to greenschist
facies, carbonaceous tuffaceous rocks, siliceous shale and carbonate
rocks. Terrane possibly interpreted as a fragment of back-arc depression
deposited on oceanic crust. Terrane structural elements are separated by
thrusts and terrane area is intruded by early Paleozoic gabbro and
granite.

**REFERENCES**: Konovalova and Prusevich, 1977; Goncharenko and others,
1982; Dergunov, 1989; Simonov and others, 1999.

## TF Tonod terrane (Greenschist) (Paleoproterozoic) (Transbaikalia)

## 

Consists of sedimentary rocks of the Kevaktinsky series that consists
from older to younger of gravelstone, metasandstone, metaaleurolite,
phyllite, and carbonaceous phyllite metamorphosed up to biotite stage of
greenschist facies. A Pb-Pb isochrone isotopic age of carbonaceous
phyllite is 2,467 Ma. Granitoids (Chuya-Nerchinsk complex) intruding
large parts of the have U-Pb zircon isotopic ages of 2,114 Ma, and a
Rb-Sr isotopic age of 750 and 735 Ma. Amphibolite facies metamorphism
and migmatite along the contacts of the granite batholiths. Also
occurring are Early Riphean dikes and minor of gabbro-diabase and
diabase. The sedimentary rocks of the terrane are folded into linear and
domal folds. Accretion of terrane to the North Asian Craton was occurred
with intrusion of granite porphyry stocks and granodiorite-porphyry of
the Yazovsky complex with U-Pb zircon isotopic age of 730. The northwest
and southeast margins of the terrane are bounded by overthrusts, and the
southwest and northeast parts of the terrane are discordantly overlapped
by Riphean sedimentary rocks of the Patom sedimentary basin.

**REFERENCES**: Bukharov and others, 1992; Sharov and others, 1992;
Ivanov and others, 1995.

## TG Tsagaan Uul-Guoershan Terrane (Continental margin arc) (Paleoproterozoic through Permian) (Mongolia, Northwestern China)

## 

In northwestern China, consists of: (1) Precambrian metarhyolite, quartz
schist, marble, quartz-plagioclase gneiss with a Rb-Sr whole rock
isotopic age of 1,755 Ma; (2) overlapping Middle Ordovician
andesite-porphyry and diabase porphyry, volcanoclastic rocks, sandstone,
mudstone, and limestone with gastropods, brachiopads and trilobites; (3)
Early Silurian graywacke, siltstone, and shale interlayered with
limestone containing graptolites; (4) Devonian calcareous sandstone,
reef limestone, chert, tuff, sandstone, and limestone with gastropods,
brarchipods, trilobites, and anthozoa; and (5) Early and Late
Carboniferous sandstone, marble with gastropods, garchipods, and
anthozoa, and siltstone, chert, rhyolite, dacite, and tuff. Terrane is
intruded by syntectonic anatectic granite and overlapped by Permian
terrigerous sedimentary rocks and volcanoclastic rocks.

**REFERENCES**: Bureau of Geology and Mineral Resources of Inner
Mongolian Aut.Reg. (Inner Mongolian GMRB), 1991; Li Wenguo, 1996;

In southern Mongolia consists of (1) Paleoproterozoic(?) schist and
migmatite, (2) Early to Middle Ordovician metavolcanic rocks,
conglomerate, sandstone, and minor limestone lenses with brachiopods;
(3) Middle to Late Ordovician conglomerate, sandstone, and minor
coral-bearing limestone; (4) Silurian limestone with brachiopods and
corals, and sandstone, siltstone; (5) Devonian pillow basalt, andesite,
tuff, sandstone, siltstone, and chert; and (6) Early Carboniferous
sandstone, siltstone with brachiopods and bryozoans, minor conglomerate.
Terrane is intruded by Middle to Late Devonian granite and granodiorite,
and is overlain by Middle to Late Carboniferous andesite, dacite, tuff,
and Permian volcanic rocks and fossil-rich limestone.

**REFERENCES**: Suetenko, 1967; Ruzhentsev and Badarch, 1985.

## TH Taukha terrane (Accretionary wedge, type B) (Late Jurassic through Early Cretaceous) (Southern Russian Far East)

## 

Consists of three overlying other tectono-stratigraphic units that are
similar in lithology and structure, but differ in rock age. Each unit is
composed of oceanic deposits, mainly chert and carbonate that grade
upward into terrigenous rocks of continental-margin origin, and
overlapping accretionary melange (olistostrome).

The low unit (Erdagou Formation) consists of Late Jurassic to Early
Cretaceous (Berriasian) chert and clay-chert overlapped Middle Jurassic
(Callovian) basalt (Erdagou suite), and Berriasian-Valanginian turbidite
deposits (Silinka suite). Thickness of chert and basalt is about 150 m
whereas thickness of terrigenous rocks is about 2,500 m. The turbidites
may be tectonically repeated. The turbidite conformably and gradually
replaces chert rocks through a section of siliceous mudstone and
mudstone. The Valanginian and Barremian accretionary melange also grades
from turbidite. The structural thickness the accretionary melange varies
from 100 to 400 m.

The middle unit (Gorbousha Formation) consists of Middle to Late
Triassic limestone (Tetyukha suite) with high-Ti alkaline basalt at the
base (400 to 500 m thick), and Early Triassic to Late Jurassic chert and
clay-chert (about 100 m thick) that grad into Late Tithonian to
Berriasian turbidite (Gorbousha suite) that grades into a
Berriasian-Valanginian accretionary melange. The thickness of turbidites
ranges from 350 to 700 m. The accretionary melange thickness is same as
above.

The upper unit (Skalistorechenka Formation) consists of Late Devonian to
Late Permian limestone (Skalistorechenka suite) associated with high-Ti
alkaline basalt (about 400 m thick), Carboniferous to Middle Jurassic
chert and overlapping Late Jurassic turbidite (Pantovyi Creek suite).
The thickness of chert and clastic deposits is not clear because of
fragmentary outcrops.

Terrane exhhibits an inverted stratigraphy with older marine formations
and overlapping terrigenous rocks (including accretionary melange)
comprising upper structural levels of terrane whereas younger units
occur at the base. However, within each structural unit, the age
succession is normal. Terrane is unconformably overlain by Late Albian
to Turonian andesite and volcaniclastic rocks of the East Sikhote-Alin
volcanic-plutonic belt.

**REFERENCES**: Khanchuk and others, 1988, Rudenko and Panasenko, 1990,
Kemkin and Khanchuk, 1993b, Kemkin and Kemkina, 1998, Kemkin and
Kemkina, 1999, 2000, Kemkin and others, 1999.

## TK Terekta terrane (Accretionary wedge, type A) (Late Neoproterozoic through Early Cambrian) (Southern Gorny Altai)

## 

Consists of a fragment of a Vendian and Early Cambrian accretionary
prism located in the Charysh-Terekta strike-slip zone. Consists of two
northwest-verging thrust sheets. (1) The lower sheet, forming most of
the terrane, consists of sanddy shale and calcareous rocks with
subordinate mafic volcanic rocks and carbonate rocks metamorphosed to
greenschist facies (Terekta suite). The upper sheet occurs as a
discontinuous band along the southern margin and consists of volcanic
rocks metamorphosed to epidote-amphibolite facies (Turgundin metamorphic
complex). Amphibolite Ar-Ar isotopic ages are 415±3 to 418±2 Ma. The
metamorphic rocks are associated with granite and granitic gneiss.
Retrograde greenschist metamorphism also occurs and occurred during
strike-slip migration of the terrane. Terrane contains small bodies of
Devonian granitoids and unconformably overlapped by Early and Middle
Devonian sedimentary and volcanogenic rocks that formed along an active
continental margin.

**REFERENCES**: Dook, 1982; Dobretsov and others, 1991; Buslov, 1992,
1998.

## TL Teletsk terrane (Accretionary wedge, type A) (Late Neoprotoerozoic) (Eastern Gorny Altai)

## 

Consists of fine-grained sandstone, siltstone, mafic volcanic rocks, and
sparse lenses of marble that are metamorphosed to greenschist facies.
Volcanic rocks occur mainly in lower part of the section. Intruded by
small late Paleozoic granitoid bodies related to collisional and
strike-slip displacement along a continental plate margin. Two types of
granite are: (1) alkaline and subalkaline granite, and (2) calc-alkaline
and plumasitic granite. K-Ar muscovite isotopic ages are 323±7 and 331±7
Ma for the Altyn-Taus subalkaline granitic massifm and a K-Ar biotite
isotopic age for schist along the contact of the massif is 343±7 Ma.

**REFERENCES**: Dergunov, 1967; Berzin, Buslov, Sintubin, 1995;
Kungurtsev, 1996.

## TM Tomsk terrane (Metamorphic) (Late Neoproterozoic) (Kuznetsk Alatau, Altai)

## 

Eastern margin of the terrane consists of complexes of Late Riphean
rocks occuring in tectonic sheets. A sedimentary and volcanogenic unit
occurs at the base (Tersin complex) and includes include metabasalt,
siliceous and carbonate rocks, and lenses of serpentinite metamorphosed
to greenschist facies. A higher sheet of mafic rocks (Konzhin complex)
is metamorphosed to greenschist to epidote-amphibolite facies.
Amphibolite exhibits a Sm-Nd isochron isotopic age of 694±43 Ma. The
volcanic rocks of the two complexes are derived from MORB and OIB types.
Amphibolite facies rocks occur in the western part of the terrane are
mainly metapelite derived from primitive crust (Tashelgin complex now
metamorphosed into garnet-bearing schist and gneiss intercalated with
marble, amphibolite, and quarztite. Terrane intruded by gabbro, diorite,
granodiorite, and granite (Sadrin and Tebin complexes) and subalkaline
leucocratic gabbro (Luzhbin complex) that stitch the tectonic sheets.
U-Pb zircon isotopic ages are 499±19 and 490±19 Ma. Late Permian and
Triassic granitoids comprise large areas and include the Tomsk
gneissogranite and granite complex with a U-Pb zircon isotopic age of
251-236 Ma, and the alkaline Porozhin monzodiorite, granodiorite,
granite, and leucogranite complex a U-Pb zircon isotopic age of 211±4
Ma. The largest plutons of these younger granites occur in shear zones
bounding the western part of the terrane. High-grade, amphibolite facies
rocks, with U-Pb isotopic ages of about 300 Ma, occur locally.

**REFERENCES**: Plotnikov, 1998; Vladimorov and others, 1998.

## TN Tokoro-Nemuro terrane (Island arc) (Late Cretaceous through Paleogene) (Hokkaido, NorthernJapan)

## 

Consists chiefly of sandstone, shale, chert, basalt, and ultramafic
rocks. Divided into an accretionary complex unit and a forearc unit.
Accretionary complex consists of accreted seamounts and sedimentary
rocks and is divided into Nikoro, Yubetsu, and Nakanogawa Groups. The
forearc unit consists of thick flysch deposits and is divided into
Campanian Saroma Group, middle Campanian to middle Eocene Nemuro Group,
and the Paleogene Urahoro Group.

**REFERENCES**: Kiminami and others, 1983, Niida and Kito, 1986.

## TO Tannuola terrane (Island arc) (Cambrian and older?) (Southern Tuva and Northern Mongolia)

## 

In the East Tannuola Range, consists of two units. (1) Marine
shallow-water and subaerial flows of basalt, andesite, dacite, rhyolite,
tuff, sandstone, siltstone, siliceous shale, and limestone (Kadvoi,
Serlig, Irbitei, and Shivelig suites). Sedimentary rocks contain Early
Cambrian archaeocyata and trilobites. (2) Sandstone and siltstone
interbedded with limestone and marl, and lesser tuffaceous sandstone and
tuff (Manailyg and Karabulun suites). Sedimentary rocks contain Middle
Cambrian trilobites. Terrane intruded by collision-related Late Cambrian
and Ordovician granitoid batholiths, unconformably overlain by
Ordovician-Silurian marine sedimentary rocks of the Khemchin-Sistigkhem
basin, and overlain by continental volcanogenic and sedimentary deposits
of the Tuva basin.

**REFERENCES**: Luchitsky, 1970; Zaikov, 1976; Volkov, 1986; Berzin and
Kungurtsev, 1996.

## TR Terpeniy terrane (Island arc) (Late Cretaceous) (Southern Russian Far East)

## 

Consists chiefly of a thick tectonic melange composed of Santonian to
Campanian deep-marine and terrestrial volcanic and sedimentary rocks
(Berozovskaya, Rakitinskaya, and Bogatinskaya sequences). Locally
contains *Inoceramus* and radiolarians. Volcanic rocks consist of
island-arc tholeiitic, calc-alkalic, and shoshonite rocks. Some basalts
are close in composition to oceanic basalt. Local abundant
peridotite-pyroxenite-gabbro and gabbro-plagiogranite intrusions are
interpreted as having formed in the magmatic chambers of the island arc.
Terrane is structurally disrupted and strongly folded.

**REFERENCES**: Geology of the U.S.S.R.; Sakhalin Island, 1970; Grannik,
1978; Khanchuk and others, 1988.

## TS Tasuul terrane (Oceanic) (Neoproterozoic) (Western Mongolia)

Occurs along western edge of Hangay upland and forms narrow (up to 10 km
by 300 km long), north-south trending allochtonous, thrust sheet to east
of Zavhan terrane. Consists of metamorphosed ophiolite composed of
ultramafic tectonite, hornblendite, metagabbro, diabase dike swarm, and
tholeiitic metabasalt that are intruded by tonalite and plagiogranite
plutons of inferred middle Riphean age.

**REFERENCES**: Makarychev, 1988; Kravtsev and others, 1989; Tomurtogoo,
1989, 1999.

## TT Telbes-Kitat terrane (Island-arc) (Neoproterozoic through Devonian) (Kuznetsk Alatau)

## 

Basal units are carbonate rocks (Kabyrzgin and Kivdin suites), and
siliceous sandy mudstone, clay-chert, carbonate rocks, and mafic
volcanic rocks (Kamzhelin and Alambai suites) of Late Riphean-Vendian
and possibly Early Cambrian age. Metamorphosed to greenschist facies,
and adjacent to faults metamorphosed to amphibolite facies. Local lenses
of serpentinitic and gabbro melange occur.

Different stratigraphy occurs in northern and southern segments. The
northern area Telbes segment consists of three units. (1) Early Cambrian
terrigenous-volcanogenic rocks, including mafic-andesite, limestone and
reef limestone of Late Aldanian and Lenian age. (2) Unconformably
overlying carbonate, volcanic,and terrigenous rocks with Amgaian fauna
(Mundybash suite). The volcanic rocks ranging from high-alkaline basalt
to rhyolite. And (3) unconformably overlying Late Cambrian and
Ordovician shallow-water marine carbonate, terrigenous, and motley
molasse (Gornoshor, Algain, and Amzas suites).

The northern, fault-bounded Zolotokitat segment consists of three units.
(1) basalt and andesite-basalt, tuff, clastic rocks, and bedded reef
limestone with Early Cambrian fauna (Edinis suite); (2) unconformably
overlying Middle Cambrian through Early Ordovician marine carbonate and
terrigenous rocks and motley molasse (Bolshekitat, Chernoosipov, Kitat,
Taimen, and Alzas suites); and (3) Middle and Late Cambriam mafic
volcanic rock and tuff, and Early Ordovician subalkaline and alkaline
volcanic rock of variable composition and pyroclastic units.

Terrane includes lens-like bodies of Vendian and early Cambrian(?)
gabbro and gabbro-diabase (Kundustuyul complex), in the Kamzhelin suite
in Zolotokitat segment. Stitching plutonic rocks are Telbes
granodiorite, quartz diorite, plagiogranite and diorite that varies from
normal to high-K calc-alkaline series (I type) with a U-Pb isotopic age
of 385±15 Ma. Granitoids are part of a Early and Middle Devonian
volcanic belt.

Locally occurring are Middle-Late Devonian(?) granite and granosyenite
intrusions (Mezen complex) in the southern area, and alkaline granite
and syenite (Kiya complex) in the northern area. Terrane is overlapped
by middle and late Paleozoic deposits of the Kuznetsk basin.

**REFERENCES:** Gintsinger and others, 1969; Alabin, 1983; Grigor\'yev,
1988; Shokalsky and others, 1997; Vladimirov and others, 1997.

## TU Tunka terrane (Island-arc) (Eastern Sayan)

## 

Occurs in southeast part of Eastern Sayan and forms a tectonic nappe
about 100 by 50 km Consists of allochthonous sedimentary rocks occurring
in the lower Urtagol and upper Toltinsky suites. (1) The Urtagol suite
contains terrigenous-volcanogenic sedimentary rocks with a basal
melange-olistostrome horizon. The lower part of the suite consists
mainly of terrigenous and terrigenous-carbonate sedimentary rocks, in
the upper part of the suite contains mainly basalt, andesite basalt, and
tuff with local often calcareous units. Suite contains bryozoans that
occur in Ordovician and younger rocks. (2) The Toltinsky suite contains
mainly carbonate and volcanic-carbonate sedimentary rocks. The carbonate
rocks consists of dolomite and limestone, locally siliceous. The
volcanogenic rocks primarily consist of calc-alkaline basalt and
andesite basalt with a sharp predominance of Na over K, a relatively
high silica content, and with a moderate total iron coefficient. Suite
also contain olistostrome layers. An Ordovician-Silurian age is defined
by conodonts and skoleocodonts. Terrane exhibits polyphase
disthene-sillimanite metamorphism adjoining the Khamar-Daban subterrane.
A Rb-Sr mineral isochron from garnet-staurolite-two-micac gneiss is
312±20 Ma. Terrane is intruded by subduction-related granitoids, and
overlapped by variegated molasse-like sedimentary rocks of the
Sagansaray suite that contains siliceous volcanic rocks (rhyodacite,
rhyolite, quartz albitophyres) contain Devonian and Early Carboniferous
plant fossils.

**REFERENCES**: Roschektaev and others, 1984; Boos, 1991.

## TY Tynda terrane (Tonalite-trondhjemite-gneiss) (Archean and Paleoproterozoic) (Yakutia)

## 

Forms a unit about 700x150 km occurs in the southern Aldan-Stanovoy
shield. Consists mostly of various Archean rocks in three complexes, the
amphibolite facies Stanovoy complex, the granulite facies Larba complex,
and the amphibolite facies Gilyui complex.

The Stanovoy complex consists of diorite-tonalite-trondhjemite gneiss,
metamafic rocks, and paragneiss (metagraywacke and metapelite).
Metamorphism is high-pressure amphibolite facies and a U-Pb zircons
isotopic U-Pb ages for tonalite-trondhjemite gneiss are 2,941±80 to
2,785±5 Ma. The age of marginal zones of zircons from the same
tonalite-trondhjemite gneiss and of zircons from metamafic dikes is
1,900 Ma which is interpreted as age of granulite metamorphism.

The Larba complex comprises relatively small tectonic slabs (up to 7,500
sq. km in area) bounded by northwest-striking faults. Tectonic wedges
have recently been mapped within the fault zone, which are composed of
metamorphosed volcanogenic and sedimentary-volcanogenic rocks of
Paleoproterozoic age (Gilyui complex). The wedges are interpreted as
fragments of the Mid-Gilyui, Unakha, and Nyukzha greenstone belts. The
Larba complex consists of enderbite and amphibole-biotite gneiss,
ultramafic schist interbedded with pyroxene gneiss and kinzigite,
calc-silicate rocks, and iron-bearing quartzite. Anorthosite and
metagabbro also occur. Metamorphism is at granulite facies of high
pressure. The age of zircons from garnet from
granite-sillimanite-cordierite gneiss is 2585± 20 Ma and is interpreted
as the age of granulite metamorphism or possibly the age of relict
zircons from the source rocks.

The Gilyui complex consists mainly of hornblende and biotite-hornblende
schist and amphibolite at the base, these lithologies and biotite gneiss
in the middle, and mainly biotite and hornblende gneiss at the top.
Complex is intruded by numerous concordant diorite and granodiorite
bodies. Metamorphism is at epidote-amphibolite facies. Pb-Pb zircons
isotopic ages for amphibolite, biotite-hornblende schist, and biotite
gneiss are 2,100 Ma and for diorite gneiss are 1,940 Ma.

An additional Paleoproterozoic complex occurs within the Djeltula fault
zone and is the Djeltula complex consisting of quartzite, mica schist,
metasandstone, metavolcanic rocks, and marble with rare metaconglomerate
layers. The complex is metamorphosed to greenschist and
epidote-amphibolite facies.

Intruding the Stanovoy and Larba complexes are granite dikes and veins
with isotopic ages of 2500 to 2000 Ma, and in the Unakha greenstone belt
are stocks of hornblende-biotite granite with an isotopic age of 1830
Ma.

**REFERENCES**: Kastyrkina, 1983; Bibikova and others, 1986; Godzevich,
1986; Mitrofanov, 1987; Moskovchenko and Kastyrkina, 1989; Nutman and
others, 1992; Rosen and others, 1994; Mironyuk and others, 1996;
Korsakov, 2000.

## TZ Tumanshet terrane (Paragneiss) (Proterozoic) (Eastern Sayan)

## 

Occurs in the northwestern part of the Eastern Sayan region and extends
for100 km long and ranges up to 70 km wide. Consists of Early or
Neoproterozoic units of: (1) a lower section of quartzite that grades
upward into high-alumina staurolite, kyanite, and chloritoid schist
interstratifed with garnet-biotite schist and calciphyre; and (2)
interlayered two-mica schist and calciphyres that grades upward into
interlayered carbonaceous and micaceous schist. Terrane intruded by
Sayan granite and unconformably overlapped by Late Riphean
terrigenous-carbonate Karagas and Oselok units and the Devonian
volcanic-sedimentary units.

**REFERENCES**: Galimova and Bormotkina, 1983; Sez'ko, 1988.

## UB Uniya-Bom terrane (Continental margin turbidite) (Late Triassic and Early Jurassic) (Southern Russian Far East)

## 

Consists chiefly of a tectonic sheet of Late Triassic to Early Jurassic
turbidite deposits and interbedded olistostromes (Amkansk, Kurnalsk,
Nelsk, and Muyakansk suites). Subdivided on basis of sandstone/mudstone
ratios and occurrence of rare fauna of *Monotis* in the Nelsk suite, and
on basis of crinoids in the Kurnalsk suite. The Late Triassic Muyakansk
suite contains an olistostrome horizon up to 500 m thick. Some limestone
lenses contain oncolite and catagraphite similar to those in the Late
Precambrian rocks of the North Asian Craton, whereas the other limestone
lenses contain Late Permian bryozoans. The turbidite deposits contain
lenses of greenstone and microquartzite typical of the
Tukuringra-Dzhagdy terrane. The sandstone and conglomerate clasts in the
Uniya-Bom terrane are partly derived from the North Asian Craton. The
Uniya-Bom terrane is intensely deformed and contains a penetrative
ductile stretching lineation that formed during strike-slip tectonic
transport. Terrane is interpreted as a forearc basin that is
tectonically linked to the Uda volcanic-plutonic belt, part of the
Mongol-Okhotsk active continental margin that occurs along the Stanovoy
block of the North Asian Craton.

**REFERENCES**: Kirillova and Turbin 1979; Natal'in and others, 1985;
Natal'in, 1993; Krasnyi and others, 1996.

## UC Ulus-Cherga terrane (Island arc) (Cambrian) (Gorny Altai)

## 

Forms an imbricated, east-verging thrust structure with various tectonic
sheets of the folowing units. (1) A basal unit of basalts and tuff
interbedded with graywacke sandstone, siltstone, siliceous shale,
jaspers and limestone with a thickness of greater than 2000 m. Upwards,
the portion of sedimentary varieties increases. Unit contains Early
Cambrian archaeocyata and trilobites. Basalt is close to MORB and partly
OIB types. Basal unit interpreted as forming over oceanic crust in a
backarc setting. (2) A structurally overlying tectonic sheet composed of
Middle Cambrian volcanic rocks, lava breccia, and basalt, and lesser
andesite and dacite, tuff with subordinate siliceous rocks, siltstone,
tuffogenic and volcanomictic sandstone. REE geochemistry suggest
formation in an island-arc. And (3) structurally overthrust Middle-Late
Cambrian fore-arc deposits consisting of polymictic and volcanomictic
sandstone, siltstone, siliceous rocks and shale with layers of
andesite-basalt tuff, tuff, conglomerate, and olistostrome. An
unconformity overlapping unit is the Early-Middle Devonian volcanogenic
and sedimentary rocks of the Altai volcanic-plutonic belt.

**REFERENCES**: Avrov, 1980; Buslov and others, 1993; Volkov, 1966.

## UG Ulgey terrane (Island arc) (Neoproterozoic through Devonian) (Mongolia)

## 

Occurs in northwestern part of Altay range and consists of a disrupted
assemblages of Vendian and Early Cambrian serpentinite melange, basalt,
andesite, tuff, and unconformably overlying Ordovician to Silurian
conglomerate, sandstone and siltstone. Terrane overlain by Devonian
volcanic and sedimentary rocks and intruded by Middle Devonian granite.

**REFERENCES:** Dergunov and others, 1980; Demin and Demin, 1993.

## UK Urik-Lya terrane (Greenschist) (Proterozoic) (Eastern Sayan)

In Eastern Sayan region extends northwest for more than 200 km long and
ranges up to 50 km wide. Consists mainly of inferred Paleoproterozoic
terrigenous-sedimentary rocks metamorphosed under moderate
pressure-temperature conditions. Sedimentary rocks are composed of
quartz sandstone, siltstone with thin to thick layers and lens of black
carbonaceous shale that predominate in the lower section. Layered
diabase, lava, and tuff-breccia occur in the middle section with
terrigenous-sedimentary rocks. Immature oligomictic sandstone and
graywacke predominate in the upper section. In the northwestern part of
the terrane these units are overlapped by tuff and basalt, andesite, and
liparite, tuff, and tuffaceous conglomerate. Terrane intruded by Sayan
granite and unconformably overlapped with by inferred Neoproterozoic
orogenic Ingashin unit that consists of unmetamorphosed conglomerate,
gritstone, sandstone, and siltstone.

**REFERENCES**: Konnikov and Travin, 1986; Belichenko and others, 1988;
Nozhkin, 1999.

In Transbaikalia region, consists of the Bolsherechensky (Ingashinsky)
suite composed of quartz-mica, cordierite-, andalusite- and
garnet-biotite schist alternating with amphibole schist and amphibolite,
metasandstone and phyllite schist, metasandstone, metatuffaceous
sandstone with interbeds of amphibolite, and metamorphosed mafic and
siliceous extrusive rocks of spilite-diabase formations, gravelstone and
conglomerate. Abundance of volcanic rocks increases to the northwest and
consist of Paleoproterozoicquartz and felsic porphyry and altered
spilite-keratophyre (Subluksky suite). Youngest unit consists of Early
Riphean coarse-clastic sedimentary rocks (Ermosokhinsky suite)

**REFERENCES**: Konnikov and, 1986; Nozhkin, 1999.

## UL Uimen-Lebed terrane (Island arc) (Cambrian through Ordovician) (northeastern Gorny Altai)

## 

Consists of the following four units. (1) Sedimentary and volcanogenic
rocks (Sarysaz suite) dominated by mafic volcanic rocks, including
siliceous and mafic tuff and tuff-breccia, and clastic carbonate rocks.
Early Cambrian sandstone, siltstone, gravelstone with limestone layers
(Ubin suite) with Aldanian trilobites and archaeocyata occurr locally.
Two suites intruded by gabbro and plagiogranite of which the largest is
the Sarakokshin massif in the central part of the terrane. (2)
Unconformably overlying sedimentary and volcanic-sedimentary units. Both
units contain coarse-clastic rocks with pebbles and boulders of volcanic
rocks and plagiogranite from the underlying unit, and olistostrome-like
horizons with carbonate olistoliths (Tyrgan and Verkhneynyrgin Suites).
Volcanogenic rocks consist of tuff, tuff-breccia, and lava with
carbonate rocks and marl with Early Cambrian trilobites and
archaeocyata. Carbonate blocks with Aldanian fauna occur in possible
olistoliths in chaotic horizons. (3) Early Late Cambrian high-alkaline
mafic volcanic rocks and tuff occur locally along with minor sedimentary
rocks inferred to have formed in back-arc environment. And (4)
unconformably overlying Late Cambrian-Ordovician shallow-water marine
molasse interpreted as forming during intensive deformation along an
active continental margin of the North Asian Craton during oblique or
transform displacement of lithospheric plates.

**REFERENCES**: Gintsinger and others, 1969; Berzin, 1979; Resolutions,
1979; Avrov , 1980; Shokalsky and others, 1997.

## UN Ulban terrane (Continental margin turbiditie) (Late Triassic through Middle Jurassic) (Southern Russian Far East)

## 

Consists mainly of Late Triassic and Early-Middle Jurassic turbidite
that is tectonicaly mixed with rare sheets of Middle Jurassic chert and
basalt. Boudinage, minor asymmetric folds with subhorizontal hinges, and
duplex structures occur. South-vergence of subduction-related folds and
thrusts occurs in most cases. Overlapping sedimentary,
volcanic-sedimentary assemblages and stitching plutonic granitoids are
as follows. (1) Early Cretaceous granite of Kharga plutonic complex; (2)
Intermediate composition Early Cretaceous volcaniclastic and volcanic
rocks; (3) Late Cretaceous bimodal volcanic and volcaniclastic rocks and
Late Cretaceous granite of the Khingan-Okhotsk volcanic-plutonic belt;
and (4) Paleogene and Neogene nonmarine clastic deposits and Neogene
basalt.

**REFERENCES**: Decision, 1990; Martynyuk and others, 1990; Natal\'in,
1993; Krasnyi and others, 1996.

## UO Ulugo terrane (Island arc) (Early Cambrian) (Tuva)

## 

Consists of variable-composition units that range up to 8 to 9 km thick.
Subdivided into Ottug-Taiga and Syynak suites or Tumat-Taiga and Tapsa
suites. Consists consists of three units: (1) a mafic volcanic unit with
subordinate siliceous volcanic rocks and tuff, siliceous rocks and black
shale, and limestone with Early Cambrian archaeocyata; (2) a siliceous
volcanic-tuff unit with subordinate mafic volcanic rocks and siliceous
shale; and (3) a tuff and sedimentary rock unit composed of tuffaceous
conglomerate, reef limestone, siliceous and mafic volcanic rocks and
tuff, sandstone. Siliceous shale occurs in the lower part and sandstone,
siltstone, limestone with Early Cambrian archaeocyata, tuff, black
shale, siliceous shale, and andesite occur in the upper part. Volcanic
and related rocks interpreted as forming in an island-arc setting by the
occurrence deep-water of pillow-lava and siliceous sedimentary rocks,
and subaerial red sedimentary rocks and. Mafic and siliceous hypabyssal
and subvolcanic bodies occur throughout the section. Unconformity
overlying are: (1) collisional-related Late Cambrian terrigenous rocks
(Tashtygkhem suite) composed of Middle-Late Cambrian collisional
granitoids; and (2) Early Devonian rift-related volcanic-sedimentary
rocks; and (3) Middle and Late Devonian continental molasse.

**REFERENCES**: Luchitsky, 1970; Zaikov, 1976; Bukharov, 1979; Berzin
and Kungurtsev, 1996.

## UR Urmi terrane (Passive continental margin) (Archean through Middle Triassic) (Northeast China, Southern Russian Far East)

Consists of (1) Middle Archean amphibolite, chert, gneiss, quartzite
(Amur series); (2) Middle Archean granite, granodiorite, gneiss-granite
and migmatite plutonic rocks of ultrametagenous type (Bureya rock
complex); (3) Middle Ordovician granite; (4) Early and Middle Devonian
marine terrigenous and terrigenous-carbonate rocks with corals,
brachiopods, bryozoans, crinoids, trilobites (Niran and Pachan suites);
(5) Early Permian rhyolite and tuff; (6) Early to Late Permian shallow
marine sandstone, siltstone and conglomerate with mixed Boreal-Tethyan
type bryozoans, brachiopods, and Tethyan-type ammonoids (Osakhtin
suite); (7) Early and Middle Triassic turbidite; and (8) Late Triassic
shallow marine deposits. Overlapping sedimentary an volcanic-sedimentary
assemblages are as follows. (1) Early Jurassic (Langary suite) and
Middle Jurassic (Budakan and Katon suites) composed of nonmarine
sandstone, siltstone with flora. (2) Early-Late Cretaceous nonmarine
sandstone, siltstone, and coal (Nabat, Bira, Chuki-Poktoi Bolshechurkin
members), and Early-Late Cretaceous andesite, rhyolite, and rhyolite
tuff forming a part of the Khingan-Okhotsk volcanic-plutonic belt. (3)
Cenozoic sandstone, mudstone, and pebble conglomerate. And (4) stitching
plutonic rocks of Late Cretaceous granite and granodiorite of the
Khingan-Okhotsk volcanic-plutonic belt.

**REFERENCES**: Resolutions, 1979; Krasni and others, 1996.

## VS Voznesenka terrane (Passive continentalal margin) (Cambrian through Permian) (Southern Russian Far East)

## 

Constitutes southwestern Khanka superterrane. Consists of four major
units. (1) Cambrian sandstone, pelitic shale, rhyolite, felsic tuff,
limestone with Atdabanian to Lenian archaeocyathidsand, and dolomite
ranging up to several thousand meters thick. Rhyolite exhibits a Rb-Sr
whole-rock isotopic age of 512 Ma. Cambrian rocks are intensely deformed
and intruded by Ordovician collision-related granitic rocks with a Rb-Sr
whole-rock isotopic age of 480 Ma. (2) Ordovician to Early Silurian
conglomerate and sandstone according to questionable flora. (3) Early
Devonian rhyolite and felsic tuff, and Middle and Late Devonian
rhyolite, felsic tuff, and rare basalt with intercalated continental
rocks and shallow-marine clastic rocks with limestone lenses, and Early
and Middle Carboniferous rhyolite, silicic tuff, siltstone, and
limestone lenses with Tethyan forminifera. And (4) Late Permian basalt,
andesite, rhyolite, sandstone, and siltstone with plant fossils.
Overlapping Mesozoic and Cenozoic volcanic and sedimentary are: (1)
Early and Middle Triassic marine clastic rocks; (2) interbedded Late
Triassic marine and nonmarine coal-bearing clastic rocks; (3) marine
Jurassic deposits with an abundant fauna; (4) Hauterivian and Albian and
younger Cretaceous clastic coal-bearing rocks that also unconformably
overlie the Laoelin-Grodekovsk and the Sergeevka terranes of the Khanka
superterrane; (5) Late Cretaceous and Paleogene calc-alkalic volcanic
rocks of the East Sikhote-Alin volcanic-plutonic belt that overlaps all
terranes of the southern Russian Far East; and (6) younger Cenozoic
deposits including Paleogene and early Neogene epicontinental
sedimentary rocks, and late Neogene alkalic basalt of the
Sakhalin-Primorye volcanic belt. The Voznesen terrane was amalgamated
with other terranes of the Khanka superterrane in the early Paleozoic,
and in the Early Cretaceous, the Khanka superterrane was accreted to the
eastern margin of Asia.

**REFERENCES**: Geology of the U.S.S.R., 1966; Goroshko, 1983; Oleinik,
1983; Nazarenko and Bazhanov, 1987; Belyaeva, 1988; Khanchuk and others,
1991; Androsov, 1992; Izosov, 1992.

## WAD West Aldan terrane (Granite-greenstone) (Archean) (Yakutia)

## 

Forms a block about 400 km by 350 km and occurs on the western margin of
the Aldan-Stanovoy shield.

Terrane consists of Archean rocks of different types metamorphosed under
widely ranging temperatures and pressures. Orthogneiss of
tonalite-trondhjemite composition predominate and form the Olekma
complex that occurs in several large linear blocks separated by four
longitudinal belts about 300 km long and 30 km wide. The belts contain
tectonic greenstone slabs of the Subgan complex; blastomylonite bounds
the belts. The Kurulta granulite complex forms several independent
fault-bounded blocks and tectonic slabs. All these blocks and zones may
be independent terranes.

The Olekma tonalite-trondhjemite complex consists of compositionally
similar biotite, biotite-amphibole, and amphibole plagiogneiss and
highly aluminous gneiss. These units are enriched in LREE and have high
Sr and low U contents. Associated are mafic schist and amphibolite
bodies. The age of tonalite-trondhjemite gneiss is 3.0 to 2.7 Ga.
Orthogneiss older than 3.0 Ga also occurs. Units are generally
progressively metamorphosed to moderate pressure amphibolite facies.
Nearby the greenstone belts, orthogneiss exhibits low-grade amphibolite
facies retrograde metamorphism with the formation of heteroblastic,
glomeroblastic, and blastomylonite structures.

The Subgan greenstone complex contain varous rock assemblages and
metamorphosed at varying degrees. Sedimentary and volcanogenic rocks in
the greenstone belts exhibit isotopic ages of 3.2 to 3.0 and 3.0 to 2.7
Ga. Contacts between greenstone belts and the surrounding rocks of the
tonalite-trondhjemite complex are generally tectonic or intrusive
contacts.

The Tokko-Khani greenstone belt contains small amounts of mafic and
ultramafic volcanic rocks in combination with siliceous and intermediate
volcanic rocks that are metamorphosed to high grade kyanite-sillimanite
type. To the west and east, the Chara-Tokko and Temulyakit-Tungurcha)
greenstone belts contain tholeiitic volcanic rocks, banded iron
formation, and carbonate-terrigenous rocks (Temulyakit-Tungurcha and
Saimagan). Two generations of greenstone belts occur one with ages of
3.3 to 3.0 Ga (Syrylyr tectonic slab) and the other with ages of 3.0 to
2.9 Ga (Olondo synform and Tasmiele wedge).

The Kurulta granulite complex comprises the Olomokit, Chara, and Kalar
blocks and consists mainly of orthoenderbite- and
charnockite-orthogneiss along with paragneiss, including amphibole- and
pyroxene-bearing gneiss and schist, garnet-biotite gneiss, rarely with
cordierite and sillimanite. The blocks form relatively thin tectonic
slabs overthrusting the tonalite-trondhjemite and greenstone complexes.
Scarce isotopic data for the protoliths of garnet-biotite gneiss of the
Olomokit block derivation from rocks with a Nd model age of 3.5 Ga; data
for the protoliths of two-pyroxene schist formed indicates derivation
from rocks with a Nd model age of 3.15 Ga. This suggests that the age of
granulite metamorphism is no older than 3.15 Ga. The upper age limit of
metamorphism is constrained by the emplacement of the Charodakan granite
complex with an isotopic age of 2.6 Ga.

Stitching assemblages include granite and pegmatite that intrude the
Archean metamorphic complexes. The granites form small orthogneiss and
migmatite bodies and large plutons up to 2,500 km^2^ in size (Charodakan
pluton). Chemical analysis indicates a normal granite series with equal
amounts of K~2~O and Na~2~O, and, less frequently, to subalkaline
granite with K~2~O slightly prevailing over Na~2~O. Granite from the
eastern margin of the Tasmiele tectonic slab exhibits an isotopic age of
2.7 Ga. The largest of the plutons, the Charodakan, is dated at 2.6 Ga.

Unconformably overlap assemblages are Paleoproterozoic medasedimentary
rocks of the Udokan and Uguy series in the Kodar-Udokan, Early Khani,
Oldongso, and Uguy graben-like basins. A U-Pb age of volcanogenic
zircons from metagraywacke and tuffaceous sandstone of the Udokan series
in the Kodar-Udokan basin is 2.18±0.005 Ga. The metasedimentary rocks
are intruded by granite of the Kodar complex with an isotopic age of
1.8-1.9 Ga. Metasedimentary rocks in the Early Khani basin are separated
from the surrounding orthogneiss by faults and consist of marmorized
dolomite, metaquartzite, and oligomictic metasandstone with conglomerate
lenses, rhythmically interlayering metapelite and metapsammite, as well
as polimictic and oligomictic metasandstone. The total thickness of is
1800 to 2100 m. Also occurring are metadiabase sills ranging up to 150
to 200 m thick. Units are metamorphosed to greenschist facies (biotite
zone), and rarely up to low-grade -amphibolite facies with isotopic ages
of 1.95±0.11 Ga. Basal deposits are well correlated with the Udokan
series in the Oldongso basin, unconformably overlap the Charadokan
granite pluton and orthogneiss of the Olomokit granulite block. Basal
units include include poorly sorted gravelstone, conglomerate,
coarse-grained sandstone, and breccia. Units are metamorphosed up to
chlorite-sericite zone of greenschist facies. Sedimentary rocks are
intruded by metadiabase sills with isotopic ages of 1.88 Ga. The Udokan
series is unconformably overlain by terrigenous rocks of the Uguy series
that consists of boulder-pebble conglomerate and grey and rose-grey
oligomictic and quartz sandstone, both massive and bedded. Occurring in
the sandstone are bands of silty sandstone and local slaty siltstone.
Bedding is thin, horizontal and oblique, and cross-wavy.

**REFERENCES**: Mironyuk and others, 1971; Neelov and others, 1971;
Petrov, 1976; Cherkasov, 1979; Kudryavtsev and Nuzhnov, 1981; Rublev and
others, 1981;Grabkin, 1982; Beryozkin and others, 1983; Bushmin and
others, 1983; Drugova and others, 1983; Aksenov and others, 1985;
Beryozkin and Smelov, 1985; Bogomolova and others, 1985; Dook and
others, 1986; Sochava, 1986; Levchenkov and others, 1987; Mitrofanov,
1987; Berezhnaya and others, 1988; Drugova and others, 1988; Gorokhov
and others, 1989; Smelov and others, 1988;Smelov, 1989; Popov and
others, 1990; Kovach and others, 1995b; Smelov, 1996; Stogniy and
others, 1996; Smelov and Beryozkin, 1997.

## WAG West Angara terrane (Passive continental margin) (Neoproterozoic) (Yenisey Ridge)

## 

Occurs in the central part of the Yenisey Ridge and extends northwest
for 450 km and ranges up to 80 km wide. Consists of Middle and Late
Riphean metamorphosed terrigenous, terrigenous-carbonate, and carbonate
sedimentary rocks of three units that formed along a passive continental
margin. High-aluminous kyanite-(andalusite-sillimanite)-staurolite
gneiss, quartz-mica schist, quartzite, and marble occur in the lower
parts of sections (Teya unit). Interstratal bodies of orthoamphibolite
occur in the upper part. The sedimentary rocks of Teya unit are
concordantly or unconformably overlapped by terrigenous and
terrigenous-carbonate sedimentary rocks of Sukhopit unit that consists
of mainly metasandstone, metasiltstone, quartz-chlorite-sericite often
carbonaceous schist, rhythmically laminated sedimentary rocks that grade
upward into limestone and dolomite. Units are metamorphosed from
amphibolite to lower greenschist facies. Autochthonous granite and
migmatite of Teya complex occur with gneiss of Teya and Sukhopit units
and has an U-Pb zircon isotopic age of 866 Ma. Teya, Sukhopit, and
Tungusik units were intruded by calc-alkaline granitoids of
Tataka-Ayakhta complex with an U-Pb zircon isotopic age of 760 Ma.
Unconformity overlapping is the Late Riphean and Early Cambrian
Vorogovka-Chapa sedimentary assemblage.

**REFERENCES**: Khomentovsky and others, 1972; Kornev and others, 1974;
Postel'nikov, 1980; Nozhkin and others, 1998; Vernikovskaya and others,
in press.

## WB Waizunger-Baaran terrane (Island arc) (Ordovician through Permian) (Northwestern China, southwestern Mongolia)

In northwestern China, consists of: (1) Ordovician limestone with
intercalated andesite, terrigenous rocks, intermediate- and mafic-tuff,
mafic- and siliceous-volcanic rocks, and muddy limestone with
trilobites, pelecypods, and corals; (2) unconformably overlapping
Silurian sandstone, conglomerate, pyroclasic rocks, and limestone with
corals and brachiopods; and (3) mainly Devonian mafic and intermediate
mafic volcanic rocks, and minor siliceous volcanic rocks and tuff,
fine-grained sandstone, siltstone, and limestone with trilobites and
brachiopods that grade into coal clastic rocks. Overlying are Permian
continental volcanic and terrigenous rocks with local coal.

In southwestern Mongolia, consists of: (1) Early Devonian tholeiite
pillow basalt, diabase, tuff, sandstone, chert, and minor limestone; (2)
Early to Middle Devonian volcaniclastic sandstone, argillite and chert,
and minor lenses of limestone with corals; (3) Middle to Late Devonian
basalt, andesite, pyroxene porphyry, shoshonite, and quartz latite; (4)
Early Carboniferous trachyandesite, quartz latite, trachydacite,
rhyodacite, tuff, sandstone, siltstone, and minor limestone with
brachiopods. Postaccretion stitch complexes are Middle to Late
Carboniferous granodiorite, gabbro, picrite diabase, granosyenite, and
Early Permian leucogranite. Rhuzhentsev and others (1989) interpret the
terrane as a fragment of a Devonian continental margin arc formed on the
thick crust, based on the composition of volcanic rocks. In contrast,
Badarch and Orolmaa (1996) and Baofu (1993) interpret the terrane as a
combination of a volcanic island arc and backarc basin**.**

**REFERENCES**: Gavrilova and others, 1975; Dergunov and others, 1980;
Badarch and Orolmaa, 1989; Bureau of Geology and Mineral Resources of
Xinjiang Uygur Aut. Reg.(Xinjiang GMRB), 1990; Ren Jishun, 1980;
Ruzhentsev and others, 1992; Han Baofu, 1992, 1993.

## WD Wundurmiao terrane (Accretionary wedge, type B) (Mesoproterozoic through Middle Ordovician) (Northern China, Mongolia)

## 

Extends to east-west and consists of : (1) A lower Mesoproterozoic
ophiolite composed of gabbro, diabase, schistose tholeiite with apparent
pillow structures and lenses of ferrous, silica-rich rocks, and an upper
Mesoproterozoic unit composed of sericite schist, sericite-quartz
schist, chlorite schist, two-mica-quartz schist, ferrous quartzite,
greenschist, marble, and glaucophane schist that comprise a suite of
radiolarian-bearing, pelagic, silica-rich ferrous rocks; (2)
Neoproterozoic sericite-quartz schist, chlorite-sericite schist,
chlorite-calcite schist, metasandstone, phyllite, and lenses of
phyllite-limestone with a U-Pb isotopic age of 1130 Ma ; (3) Early and
Middle Ordovician altered andesite, chert, marble-like slate, altered
basalt, tuff, and volcanic breccia; tuff contains radiolarian,
graptolites and foraminifera. Terrane intruded by granodiorite porphyry
with a U-Pb isotopic age of 466 Ma, and is unconformably overlain by
Silurian marine terrigenous clastic rock.

**REFERENCES**: Bureau of Geology and Mineral Resources of Inner
Mongolian Aut.Reg. (Inner Mongolian GMRB), 1991; Hu Xiao, 1986; Li
Jinyi, 1987; Wang Quan, 1991; Chen Qi, 1992; Zhang and Sklyarov, 1992;
Li Weiguo, 1996.

## WSA West Sakhalin terrane (Accretionary wedge, type A) (Cretaceous) (Southern Russian Far East)

## 

Consists chiefly of: (1) a basal sequence of Early Cretaceous volcanic
rock, jasper, and pelagic rocks (Samokhinskaya, Pobedinskaya, and
Tymovskaya sequences); and (2) Late Cretaceous clastic and tuffaceous
clastic rocks with *Inoceramus* and ammonites (Arkovskaya and
Krasnoyarkovskaya sequences). The Late Cretaceous rocks are interpreted
forearc trough deposits and are overlapped by Tertiary conglomerate and
sandstone. Terrane deformed into northwest-striking folds and is
interpreted as a forearc basin that formed along the igneous arc formed
by the East Sikhote-Alin volcanic-plutonic belt. Terrane correlated with
Sorachi-Yezo terrane on Hokkaido Island in northern Japan. For
paleomagnetic determinations, three Late Cretaceous localities exhibite
poor-quality southerly displacements of 5o[+]{.underline}10o,
12o[+]{.underline}7o and 20o[+]{.underline}3o with respect to the
Siberian platform. Best estimate suggests displacement to the south of
about 15o.

**REFERENCES**: Geology of the U.S.S.R., Sakhalin Island, 1970;
Pechersky, 1970; Parfenov, 1984; Zyabrev, 1984; Nevolina and Sokarev,
1986.

## WST West Stanovoy terrane (Metamorphic) (Archean through Mesoproterozoic) (Transbaikalia, Mongolia)

## 

In Mongolia, consists of Precambrian(?) gneiss, migmatite, amphibolite,
quartzite and marble, minor pegmatite and diabase, and porphyry dikes
with K-Ar isotopic ages of 2,650, 2,480, 1200to 2200 Ma. A f oliated
granite exhibits a K-Ar isotopic age of 89-129 Ma. Overlap assemblage
consists of Permian subalkalic volcanic and volcaniclastic rocks.

**REFERENCES:** Koval and Smirnov, 1983; Kozakov, 1986; Zorin and
others, 1997; Tomurtogoo and others, 1999.

In the Transbaikalia region, consists of several sequences.

Oldest Archean and Paleoproterozoic units are Early Archean Mogocha,
Late Archean Nikitkinsky, and Paleoproterozoic Tungirsky metamorphic
complexes that consists of schist, gneiss, quartzite-aluminous and
carbonate subcomplexes metamorphosed to granulite facies. The granulite
metamorphism has a U-Pb zircon isotope age of 1.9 Ma. Intrusive rocks
consist of the Early Archean upper Moklinsky complex with a Rb-Sr
isotope age of 2.6 to 2.9 Ma, Late Archean Amazar and Early Stanovoy
complexes, and Paleoproterozoic Oloshkinsky Late Stanovoy complexes in
which granitoids predominate significantly over mafic plutonic rocks.
Southwest part of terrane consists of Precambrian(?) gneiss, migmatite,
amphibolite, quartzite and marble, minor pegmatite and diabase and
porphyry dikes interpreted as a metamorphic core complex formed during
early Creataceous continental extension. K-Ar isotopic ages for
mylonitic foliated granite are 89 to 129 Ma.

Several younger units also occur. (1) The Middle Riphean Irgainsky suite
composed of metabasalt, greenschist, marble, and phyllite with
interlayered metasandstone, quartzite, conglomerate; and subconcordant
dikes of basalt and andesite. (2) The Cambrian Solontosvsky
volcanic-sedimentary sequence contains late Riphean and Cambrian
microfossils and consists of sedimentary rocks composed of sandstone,
aleuropelite, conglomerate, and marble, and volcanic rocks composed of
rhyolite, trachyrhyolite, dacite, andesite, basalt, and intermediate and
siliceous tuff. The intrusive equivalents are the layered mafic and
spare ultramafic rocks of the Kruchininsky complex, and granitoids of
the Krestovsky complexes with an inferred early Paleozoic age. Younger
batholith intrusions of quartz-diorite, granodiorite, and granite
exhibit a Rb-Sr isotope age of 438±7.6 Ma and are the product of
palingenic melting.

Overlap and stitching complexes the Barguzin-Vitim batholith, Selenga
sedimentary-volcanic-plutonic belt, and Trans-Baikalian-Daxinganling
sedimentary-volcanic plutonic belt that indicate pre-late Carboniferous
accretion of the terrane to the North Asian Craton.

**REFERENCES**: Koval, Smirnov, 1982; Vinogradov and others, 1983;
Kozakov, 1986; Bibikova and others, 1993; Anashkina and others, 1997;
Zorin and others, 1997; Tomurtogoo and others, 1999; Kazimirovsky and
others, 2000.

## WSY West Sayan terrane (Continental margin turbidite) (Late Neoproterozoic through Devonian) (Western Sayan and eastern Gorny Altai)

## 

Consists of several large tectonic sheets and lenses ranging up to 50 km
or more wide. Sheets are separated by complicated strike-slip and
inbricated-thrust zones and constitute subterranes. Terrane may be
underlain by Vendian and Early Cambrian ophiolite and accretionary units
that are exposed along the terrane periphery and in a tectonic window.
The terrane consists mainly of thick Cambrian-Ordovician sand-shale
flysch that are overlapped by Silurian shallow-water
carbonate-terrigenous shelf deposits, and by Devonian and Early
Carboniferous continental volcanogenic and terrigenous rocks. The major
units, from oldest to youngest, are as follows. (1) Late Precambrian or
Cambrian sandy-silty shale of the Syutkhol and Ishkin suites with
typical sparese quartz and plagioclase clasts. The coarse-clastic rocks
increase upsection and become more polimictic. (2) Overlapping Cambrian
coarse-clastic, polymictic and motley sedimentary rocks, and andesite,
granitic pebble conglomerate, and flysch. (3) Ordovician flysch, mainly
sandstone and shale (Shignet series). The proportion of sandstone,
siltstone, and shale varies greatly. Calcareous rocks, shale, marl, and
sandy limestone constitute a major part of the Late Ordovician section.
Local brachiopods, corals, and trilobites occur. Also occurring are
exoticOrodvician chert, jasper, and quarztite in the northern part of
the terrane. (4) Conformable to unconformable overlying Early Silurian
rocks are carbonate rocks with reef containing abundant corals,
crynoids, brachiopods, and trilobites (Onin and Yaryshkol suites), and
terrigenous interbedded motley sandstone, siltstone, and mudstone
(Taslin suite). (5) Unconformably overlying in the southern part of the
terrane are Late Silurian motley marine molasse composed of cross-bedded
sandstone, siltstone, and conglomerate with unevenly distributed
limestone interbeds with brachiopos and corals. And (6) Early Devonian
continental terrigeous-volcanic rocks, and lesser Carboniferous through
Jurassic coal-bearing molasse that fills fault graben basins.

Most of the terrane is metamorhosed to greenschist and
prehnite-pumpeliite facies of. Late Ordovician and Silurian units are
less or not metamorphosed. Locally, metamorphism attains amphibolite
facies. K-Ar isotopic age of metamorphism granite, migmatite, gneiss,
and schist is Devonian and Early Carboniferous. Early Devonian or Early
Silurian plutons intrude areas metamorphosed to greenschist facies and
consist of a tonalite-granodiorite complex (Bolshoy Porog complex), and
a REE subalkaline granite-leucogranitic complex with granosyenite and
syenite (Dzhoy complex).

**REFERENCES**: Zonenshain, 1963; Dergunov, 1967; Kheraskov, 1979;
Berzin, Dobretsov, 1994; Buslov, Sintubin, 1995; Zonenshain and others,
1990.

## XC Xichangjing terrane (Metamorphic) (Proterozoic) (Northwestern China)

## 

Extends east-west and mainly consists of two suites of metamorphic
rocks: (1) Mesoproterozoic, low- and middle-grade metamorphosed clastic
rocks interlayered intermediate to ultramafic volcanical rocks; and (2)
Neoproterozoic low-grade metamorphosed clastic rocks and interlayered
carbonate rocks and chert.

**REFERENCES**: Zuo Guoquan and others, 1990; Bureau of Geology and
Mineral Resources of Inner Mongolian Aut.Reg. (Inner Mongolian GMRB),
1991; Bureau of Geology and Mineral Resources of Gansu province (Gansu
GMRB), 1991; He Guoqi and others, 1994.

## YN Yenisey terrane (Paragneiss) (Paleoproterozoic?) (Yenisey Ridge)

## 

Extends in a submeridional direction for 200 km long and ranges up to 30
km wide. Consists of in ferred Paleoproterozoic volcanic-terrigenous
units metamorphosed to amphibolite facies. From west to the east,
metamorphosed terrigenous-carbonate rocks with tholeiite basalt grade
into differentiated calc-alkaline rocks ranging from rhyolite to dacite
to basalt, and associated mature metasedimentary rocks. Volcanic and
sedimentary rocks metamorphosed to gneiss and mica-quartz schist with
interlayered quartzite. Units interpreted as a margin basin of an
ensialic island arc and associated continental slope and foot deposit.

**REFERENCES**: Bibikova and others, 1993; Nozhkin, 1999**.**

## ZA Zavhan terrane (Continental margin arc) (Late Neoproterozoic) (Mongolia)

Occurrs in northern and southern segments separated by Hangay fault. The
northern segment extends for 450 km and ranges up to 90 km wide, and the
southern segment extends longitudunally for 350 km and ranges up to 130
km wide. Consists of Riphean complexes, from east to west, interpreted
as forming along an active continental margin: (1) Zavhan-Mandal
batholith of calc-alkalic diorite, tonalite and palgiogranite with a
K-Ar isotopic age of 840 Ma; (2) Hutul-Hasagt fold- and thrust-belt
containing Alpine type ultramafic rocks, a spilite-keratophyre bimodal
series, and carbonate-siliceous rocks, and phyllite, (3) Urgamal fold
belt containing calc-alkalic basalt, rhyolite, tuffaceous flysch,
carbonaceous slate with stromatolites, and limestone; and (4)
Buural-Darive imbricated fold zone, containing thick
quartzite-carbonite-schist complex with blocks of early Precambrian
schist and Riphean(?) Alpine-type ultramafic rocks and mafic volcanic
rocks. Most of complexes overlapped by late Late Riphean volcanic
molasse (Zavhan formation) occurring in a rift structure. Terrane is
overlain chiefly by Vendian to Early Cambrian carbonate- terrigenous
sedimentary rocks and stitched by Late Cambrian granitoids.

**REFERENCES**: Geologic Map., 1987, 1999, Map., 1989, Tomurtogoo, 1989,
1990.

## ZN Zhangguangcailing superterrane (Continental margin arc) (Neoproterozoic through Devonian) (Northeastern China)

## 

Extends north-south and consists chiefly of the following units. (1)
Paleoproterozoic basement containing schist, quartzite, marble, and
gneiss (Xinhuadukou Group). (2) Neoproterozoic tuff, rhyolite dacite,
slate, shale, quartzite, marble and metamorphic sandstone (Yimianpe and
Dongfenshan Groups). (3) local Neoproterozoic and Early Cambrian
siliceous slate, limestone, marble, carbonaceous slate and siltstone
(Xilin Group), and local Ordovician sedimentary deposits and
intermediate-mafic volcanic rocks. The Early Ordovician rocks include
limestone, conglomerate, lava, and tuff. The Late Ordovician rocks
include mafic-intermediate lava (over 530 m in thickness), sandstone,
siltstone and slate. (4) local overlapping Devonian carbonate, and
terrigenous and felsic rocks (Xiaobeihu, Fuxingtun, Hongchuan, and
Heilonggou Formations). And (5) late Paleozoic, Mesozoic, and Cenozoic
overlap assemblages. Synorogenic Ordovician and Silurian plutons intrude
the superterrane that is extensively intruded by Hercynian and Mesozoic
plutons. Local blueschist metamorphism with Na amphibole (crossite) and
glaucophane.

**REFERENCES**: Dong and others, 1985; Heilongjiang GMRB, 1993; Maruyama
and others, 1996; Zhao Chunjin and others, 1996; Krasnyi and others,
1996; Sun Jiapeng and others, 2000.

## ZO Zoolen terrane (Accretionarry wedge, type B) (Ordovician(?) and Devonian) (Mongolia)

## 

Ranges up to 30 km wide and extends for 700 km in southern Mongolia and
consists of several tectonic sheets, slivers, blocks, and melange units
of mainly Ordovician(?) to Devonian tholeiite basalt, andesite, tuff,
volcaniclastic rocks, and chert metamorphosed to greenschist facies.
Also occurring are scattered small ultramafic bodies, and serpentinite
melange with blocks of gabbro, peridotite, diorite, diabase, chert, and
limestone. Terrane overlain by Carboniferous volcanic rocks and flysch.

**REFERENCES:** Suetenko, 1967; Zonenshain and others, 1975; Ruzhentsev
and others, 1985.

## ZRA Zhuravlevsk-Amur River terrane (Continental margin turbidite) (Late Jurassic and Early Cretaceous) (Southern Russian Far East)

## 

Forms a S-shaped unit occurring along a major strike-slip fault system.
Southern part consists mainly of: (1) Late Jurassic chert and basalt
formed in an upper oceanic crust environment; and (2) a thick continuous
sequence of Early Cretaceous shelf and turbidite depo (up to 13,000 m
thick) derived from both oceanic and continental units. Source area for
turbidited are granitic and metamorphic rocks to the west and east of
turbidite basin. Northern part of terrane contains large open folds,
whereas appressed folds and thrust faults occur in southern and central
parts. Along the Amur River, the northern part of the terrane consists
mainly of Neocomian turbidite. Terrane intruded by Early Cretaceous
high-alumina granitic rocks with K-Ar ages of 100 to 120 Ma, and by of
the Late Cretaceous and Paleogene granite rocks of the East Sikhote-Alin
volcanic-plutonic belt. Terrane is interpreted as forming along a
transform plate boundary in the Neocomian and as a back-arc basin for
the in Kema arc in the Aptian-Albian.

**REFERENCES**: Krasny, 1966; Bersenev and others, 1969: Martynyuk and
others, 1983; Nazarenko and Bazhanov, 1986: Markevich, 1971: Golozubov
and Khanchuk, 1995.

## ZS Zasurin terrane (Oceanic) (Late Cambrian and Early Ordovician) (Northwestern Gorny Altai)

## 

Forms a folded tectonic sheet surrounded by strongly deformed
sedimentary units and consists of chert, shale, jasper, hematite
quarztite, sandstone, tuffaceous sandstone, siltstone, tuff-breccia, and
mafic pillow-lava (Zasurin suite). Volcanic rocks are associated with
diabase and gabbro-diabase bodies and are low-K, oceanic tholeiite and
oceanic island basalt. Terrane interpreted as a sedimentary-volcanic
layer of oceanic crust. Conodonts and radiolaria defines a Late Cambrian
and Early Ordovician age. The Zasurin, Talitsk and Maralikha terranes
are intruded by Late Devonian calc-alkaline and plumasitic granitoids
with U-Pb zircon ages of 365±5, 364±8, 367±4, 364v16, 371±15 Ma, and by
Late Permian and Early Triassic REE metal granite.

**REFERENCES**: Zonenshain and others, 1990; Iwata and others, 1997;
Shokalsky and others, 1997; Vladimirov and others, 1997; Buslov and
others, 1999, 2000.