Geodynamic Evolution of the East Asian Continental Margin in the Mesozoic Exempliﬁ Ed from the Bureya Basin

The Geological Society of America Special Paper 513 2015

Geodynamic evolution of the East Asian continental margin in the Mesozoic exempliﬁ ed from the Bureya Basin

Galina L. Kirillova Elena P. Razvozzhaeva Yury F. Manilov Institute of Tectonics and Geophysics, Far Eastern Branch Russian Academy of Sciences, Khabarovsk 680 000, Russia

ABSTRACT

The Bureya sedimentary basin, which is located in southeastern Russia, extends north-northeasterly for 230 km. The basin, commonly ~65 km wide, contains thick sections of Mesozoic strata that record important tectonic and eustatic changes at the edge of the East Asian continental margin. It initially developed within the passive early Mesozoic continental margin. Later, during the Late Jurassic, the basin again was strongly affected by extension. Based on up-to-date geological and geophysical data, a sequence stratigraphic model consisting of six megasequences and several sequences was constructed. Sedimentation rates, some of which are remarkably high, were calculated for each sequence. The principal evolution stages of the Bureya Basin of compound (hybrid) type are as follows: (1) During Late Triassic to Middle Juras- sic, the basin formed on the passive continental margin with edge submeridional rifts. The sedimentation was inﬂ uenced by erosion of an active continental margin. (2) Dur- ing the Late Jurassic through Cretaceous, it was an intracontinental, NE-trending, pull-apart basin.

INTRODUCTION Bureya Basin extended south as far as the Suibin (China) subbasin of the Sangjiang–Middle Amur Basin, where Middle to The Bureya sedimentary basin lies between the Bureya Mas- Upper Jurassic marine sediments have been drilled. sif and northeastern margin of the Sikhote-Alin orogenic belt, Cover rocks of the Bureya Massif consist of deformed Lower extending northerly for a distance of 230 km with an average Cambrian and Middle and Upper Paleozoic units preserved in width of 65 km (Fig. 1). The Bureya Massif in the studied area isolated troughs (Vas’kin et al., 2009). is represented by the East Bureya basement protrusion, consist- The western Sikhote-Alin fold system is composed of Meso- ing of the Turan and Lesser Khingan blocks, transected by NW- zoic turbidite, siliceous-volcanogenic units, and other marine striking faults of Early Cretaceous age. Small exposures of Mid- strata contorted into disharmonic folds. dle Jurassic strata overlying Ordovician granitoids of the Lesser However, details about the structure of the Bureya Basin Khingan block (Fig. 2) indicate that during the Mesozoic, the and its geodynamic evolution are not available. The advance of

Kirillova, G.L., Razvozzhaeva, E.P., and Manilov, Yu.F., 2015, Geodynamic evolution of the East Asian continental margin in the Mesozoic exempliﬁ ed from the Bureya Basin, in Anderson, T.H., Didenko, A.N., Johnson, C.L., Khanchuk, A.I., and MacDonald, J.H., Jr., eds., Late Jurassic Margin of Laurasia—A Record of Faulting Accommodating Plate Rotation: Geological Society of America Special Paper 513, p. 1–XXX, doi:10.1130/2015.2513(16). For permission to copy, contact [email protected]. © 2015 The Geological Society of America. All rights reserved.

1 2 Kirillova et al.

132°E 130°E 140°E 1 MONGOL-OKHOTSKMONGOL-OKHOTSK Og 0 100 200 km FOLDFOLD R.R. Bureya Basin 3 Kerbi R. R.

Bt SYSTEMSYSTEM Amgun 50°N

L 2 T

M F N NA 52°N E Amur R.

I I

T Khabarovsk L

S S R. ALIN A ALIN GI R. China Y Sungari

Japan Sea S UB Bureya S Ussuri S SYSTEM 130°E 140°E TuT A uyunyu R. n R. Chegdomyn R. Bureya Massif; blocks are Turan (Tr),

n MASSIF M 4 Urgal R. MAR Lesser Khingan (LKh) Tr Amgu Fragments of the massif cover CChh

Kn A Mongol-Okhotsk fold system B TROUGH Sikhote-Alin fold system EY

E Sn Marginal uplift; blocks are

- Chegdomyn (Ch), Gudzhal (G), R G E Synchugin (Sn), Ulkun (U)

BUR T D Urmi marginal trough; Kukan Urmi R. O

Gd L depression (Kk) B B U R E YM A H O

K KHOTE- Bureya marginal trough; depressions FOLD FOLD F LKh 5 I are Upper Bureya (UB), Sivack (S), S Gudzhick (Gd), Birsky (Br), U Kyndal (Kn), Batursky (Bt) a T (a) Deep faults of the marginal suture Kk 2 b are Tastakh (T), Kukan (K); (b) other Bira R. 6 Br deep faults (numbers in circles) are Birobidzhan South Tukuringra (1), Paukan (2), Syugdulkin (3), Melginsky (4), Khingan (5), Kharpi (6) a Cretaceous and Cenozoic formations 25 50km 0 25 b of orogenic and plate complexes: volcanogenic (a) are Badzhal (B), Ogodzha areas (Og); sedimentary (b)

Figure 1. Structural position of the Bureya Basin from Kirillova and Khanchuk (2012). Geodynamic evolution of the East Asian continental margin in the Mesozoic 3

Figure 2. Geologic map and stratiﬁ ed formations. 4 Kirillova et al.

plate-tectonic concepts has drawn increased attention to investi- The Kyndal graben is considered to be the most com- gation of the geodynamic evolution of sedimentary basins, par- pletely studied structure in the Bureya Basin. In the 1990s, ticularly oil-and-gas–bearing ones (Allen and Allen, 1990; Bally, seismic surveys and drilling were carried out, seismic- 1975; Bally and Snelson, 1980; Busby and Ingersoll, 1995; Dick- geological sections were constructed, and structural lows and inson, 1974, 1976; Fischer, 1975; Welte et al., 1997; Nitrouer, uplifts were revealed (Fig. 3), as investigated by deep drill- et al., 2007). Additionally, because of the considerable coal ing. In the northern part of the graben, the Urgal depression, reserves contained in the Bureya Basin, many economic studies containing ~4.5 km of strata, is bounded by the Kyndal fault also have been conducted over a long period of time. The basin zone on the west and an uplift on the east. The eastern uplift, has attracted increased attention over the past years in the context 5–7 km wide, extends for a distance of 30 km in the northern of oil and gas exploration, during which the latest geological and and central parts of the graben. On the east, the uplift is lim- geophysical methods were employed. ited by the Urgal fault zone, which is characterized by vertical The location of the basin at the edge of the East Asian displacement of 1.5 km. At the margin of the Eastern uplift, continental margin, where all the Mesozoic transgressions and within the Urgal fault zone, several local, gentle, anticlinal regressions have taken place, enables successful construction structures have been recognized. of a sequence stratigraphic model for the basin and recognition The central part the Kyndal graben has a maximum width of of transgressive series of black shales. Numerous global and 17 km. The faults bounding it are thrust faults that bound an uplift regional events are recorded by the sedimentary systems and formed at the latest stages of graben evolution. In the central part basins. These include unconformities, shifts of the sedimentation of the Kyndal graben, the Soloni sag (subsidence) is complicated depocenter, and changes in the structural plans at different stages by a local anticlinal structure, the Western Soloni anticline, in the of the basin evolution. As a result, the basins have become com- west. The central subsidence and Dublikan anticlinal structure posite, hybrid structures composed of several stages with various are separated by a gentle monocline. structural plans. The southern part of the graben narrows to 10 km. Numer- In the present-day structural plan, on the geological map of ous faults and anticlinal and synclinal structures suggest that the Bureya Basin (Fig. 2), one may clearly observe an eastern, the southern Kyndal graben records a contractional tectonic Lower–Upper Jurassic, pre-Kimmeridgian subbasin of nearly overprint, similar to the north. The southern edge of the central meridional trend and a Volgian–Upper Cretaceous subbasin subsidence is complicated by two anticlinal structures: western having a northeastern trend, in which the Kyndal graben is dis- Adnikan and Adnikan, with an amplitude of 200 and 500 m, tinguished (Reinlib, 1987). The Bureya Basin is overlain and correspondingly. The latter is developed above a steep, reverse intruded by Early to Late Cretaceous volcano-plutonic sequences fault, called the Adnikan thrust, which is parallel to the Urgal in the Ogodzha area to the north and in the Badzhal area to the NE-directed boundary fault. southeast (Fig. 1). Based upon integrated geological and geophysical data, a generalized seismic profi le and a map of the sedimentary DEEP STRUCTURE AND COMPOSITION OF cover thickness have been constructed. Numerous differently THE BASIN oriented seismic boundaries beneath the basin to a depth of 50 km (Fig. 4) and many faults at the surface, some of which are The deep structure of the Bureya Basin has been investigated active, provide access to deep fl uids that may have infl uenced by means of two depth-sounding profi les, gravity and magnetic the hydrocarbon formation. Eight grabens containing sections prospecting, refl ection seismology, and structure and prospect 2–4 km thick and four grabens containing sections ~2 km thick drilling. Interpretation of the geophysical data obtained has led have been recognized in the Upper Bureya and Gudzhik Basins, to better understanding of the subsurface structure of the Bureya respectively (Fig. 5). Basin (Kirillova and Khanchuk, 2012). The basement in the fl oor of the Mesozoic basin is diverse in structure and is made up of an STRATIGRAPHY Archean granite-gneiss complex overlain by Riphean to Paleo- zoic sediments cut by granitoids with diverse ages. The East Asian continental margin, which was formed in Gravimetric data reveal two graben sets, the eastern submeridi- the Mesozoic, records global subglobal Pacifi c and regional onal set and the NE-trending Kyndal set, which are separated by processes. Stratigraphy of the Upper Triassic strata and Juras- a horst. Within the eastern set, three grabens—Iorek, Eastern, and sic marine sediments in the Bureya Basin, a principal focus Adnikan, dissected by transverse faults—are recognized. The thick- of this report, was studied during large- and medium-scale ness of the sedimentary fi ll is 2800, 3200, and 2800 m, respectively. geological prospecting (Anoikin, 2004, 2004; Turbin, 1994) The Kyndal graben, which occupies almost half of the Bureya coupled with biostratigraphic investigations (Sei et al., 2004; Basin and characterizes its Cretaceous history, also consists of three Sei and Kalacheva, 1980). One of the latest versions of the grabens: Ust-Niman (3600 m), the largest Kyndal (3600 m), and basin stratigraphy, outlined next, was presented by Vas’kin et Chekunda (2400 m), separated by faults. al. (2009). 0 -4 -5 -3 -1 -2 Geodynamic evolution of-6 the East Asian continental margin in the Mesozoic 5 I 55 H, km II NNE I’ 9 2 8 7 3 5 6 1 4

l b

1 ir km

kn 50

3 , km

2 -

- 0

-K

m-K

3 Jt I H H,

11 borehole.1A (3167 m) b a

K a K c b a Urgal subsidence 45 l, A—Adnikan), b—minor; 8—borehole, its l, 2-3 reduction plane Jtl? km 0 -4 -3 -1 -2 500 250 H, A, m E 31 40 J-Kur g) + 19 kn m 1-2 U 1 I K The cutout of reflection zone 18 35 1 17 K (cg+cm) (3459 m) borehole 1S g 16 1 1 1 2-3 2-3 31 Jtl K Kir Jtl ecting horizons: a—key sections and their number, b—others, c—inferred; 2, sections and their number, ecting horizons: a—key Km J-Kur (3459 m) borehole 1S 30 Eastern Uplift (Dublikan-Soloni) 2 Jel? Eastern uplift (Dublikan-Soloni) (544 m) 1 distance, km 13 14 15 Kir 11 borehole 14- CK 1-2 K m+K g 31 Kkn J-Kur 25 A 31 J-Kur 11 12 II 1 Kir B kn 20 1-2 1 K (cg+cm) 2-3 Jtl? 910 Central subsidence A 8 1-2 Soloni subsidence Kkn 15 1 1 Kir 7 Kir 11 K m+K g 31 6 J-Kur (3167 m) borehole 1A Adnikan Uplift 5 10 I I 4 31 1 J-Kur Kir 1 3 K (cg+cm) I I El'ga Trough 5 1 Kir 2 kn 1-2 I Constructed by L.A. Tokareva (1994), modified by E.P. Razvozzhaeva (1994), modified by E.P. Tokareva Constructed by L.A. 1 31 K J-Kur Constructed by E.P. Razvozzhaeva Constructed by E.P. I’ The cutout of reflection zone II I ,km SSW 0 0 0 W 0 H 0 -1 H,km -2 -4 -3 -1 -4 -5 -3 A, m -2 400 200 level level sea Figure 3. Longitudinal (A) and transverse (B) seismogeological sections of the Kyndal graben. 1—reﬂ (B) seismogeological sections of the Kyndal Figure 3. Longitudinal (A) and transverse U—Urga major (K—Kyndal, 3; 7—faults: 4; 6—deposits of megasequence 5; 4, 5—deposits of megasequence deposits of megasequence 3— b—from a reduction plane +250 m. number and depth; 9—depth: a—from the sea level, sea 6 Kirillova et al.

Bureya Basin

NW SE 100 300 500 700 900 1100 km 0

10 K1

20 K2 30 M 40

H,km

1 2 34

Figure 4. Integrated seismic profi le from depth-sounding and refl ection profi ling (after V.A. Bormotov, 2007, personal commun.). 1—seismic discontinuities; 2—conventional seismic discontinuities; 3—dislocation with a break in continuity; 4—Moho discontinu-

ity. K1—Lower Cretaceous; K2—Upper Cretaceous.

Triassic (Late Norian) Demkukan Sequence The Taksa sequence (J1tk) is developed in the eastern part of the Gudzhik trough (675 m thick) and at the southwestern end of The Demkukan sequence, confi ned to uplifted Cretaceous the Sivak trough (1020 m thick). The sequence is mainly arkosic tectonic blocks, consists of diverse pebble sedimentary brec- and inequigranular graywacke sandstone (30–130 m) with com- cia, arkosic sandstone, graywacke, fi ne to coarse gravelstone, mon beds and layers of siltstone, gravelstone, and conglomer- and less common siltstone. The sequence discordantly over- ate. The Taksa sequence conformably overlies the Khavagda lies the Paleozoic and Proterozoic rocks of the basement. Its sequence in the Gudzhik trough. Judging from the presence of thickness varies from 350 to 700 m. The late Norian age of the conglomerate and gravelstone up to 120 m thick, the bound- Demkukan sequence is based on fi ndings of the Monotis spe- ary is eroded in the Sivak trough. The age of the sequence was cies. According to determinations by E.P. Brudnitskaya (1980, determined by E.P. Brudnitskaya as late Sinemurian based on the personal commun.), they are represented by Monotis ochotica remains of Arctomytiloides aff. rassochaensis Polub. and Serioc- (Keys.), Monotis ochotica densistriata Tell., Monotis zabaika- rinusex gr. subangularis (Miller) (Sei et al., 2004). lica Kipar., Monotis zabaikalica planostata Kipar., and Monotis The Desh Formation (J1dš) extends as narrow intermittent zabaikalica semiradiata Ich. (Anoikin, 2004). (mostly fault-bounded) strips along the western boundary of the Chegdomyn protrusion of the basement and outcrops on limbs of Early Jurassic Khavagda Sequence an asymmetric dome-shaped fold. On the eastern limb of the fold, the Desh Formation conformably overlies the Taksa sequence.

The Khavagda sequence (J1hv), which is mostly Sinemu- (Anoikin, 2004). It should, however, be noted that the absence of rian, is developed mainly in the Gudzhik trough, where it rests early Pliensbachian fauna and the transgressive basal conglomer- upon the Demkukan sequence or basement rocks. The sequence, ate, gravelstone, and sandstone beds (up to 200 m thick) extend- which accumulated following a 10 m.y. hiatus, is mainly com- ing from the southern Primorye zone to the eastern Transbaikal posed of siltstone. The subordinate components are represented region testify to an early Pliensbachian hiatus (Sei et al., 2004). by fi ne- to medium-grained arkosic sandstone along with layers The Desh Formation rests upon the basement of the western limb of lithoclastic andesite tuff, crystal-vitric felsic tuff, and rare lime- of the fold in the Gudzhik trough and in some sectors of the east- stone lenses. The sequence is 1250 m thick. The estimation of ern margin of the Bureya trough. its age is based on fi ndings of the remains of Arctomytiloide aff. The Desh Formation mainly consists of siltstone (com- rassochaensis Polub., Otapiria limaeformis (Tuchk.), and Ota- monly sandy) with beds of the arkosic sandstone and graywacke, piria affecta Polub. According to E.P. Brudnitskaya, these species as well as layers of tuffaceous siltstone and mudstone. The base indicate a Sinemurian age (Anoikin, 2003, 2004). The age of the of the Desh Formation includes a horizon, 10–150 m thick, fauna was later refi ned as late Sinemurian (Sei et al., 2004). alternating with lenticular bodies of conglomerate, gravelstone, Geodynamic evolution of the East Asian continental margin in the Mesozoic 7

Figure 5. Map of the sedimentary cover thickness.

and poorly sorted sandstone. A typical section of this formation estimated as late Pliensbachian–early Toarcian (Anoikin, 2004; may be compiled from exposures in quarries, from debris along Sei et al., 2004; Sei and Kalacheva, 1980). the Baikal-Amur mainline (BAM) railway tracks, and in the banks of the Bureya and Soloni Rivers (Anoikin, 2004; Sei and Middle Jurassic (Aalenian to Bathonian) Formations Kalacheva, 1980). The maximum thickness of the formation is 730 m. In the northern part of the basin (52°N), where the for- Middle Jurassic rocks are the most widespread in the Bureya mation attains only 350 m thickness (Sei and Kalacheva, 1980), trough. Based on the lithology and organic remains, they are sub- sandstone and less common pyroclastic units are the main divided into the Sinkal’ta, Epikan, El’ga, Chagany, and Talyn- lithologies (Anoikin, 2004). In the southern part, the forma- dzhan Formations. tion is rich in sandstone and siltstone containing plant detritus. The Sinkal’ta Formation (J2sn) overlies the Desh Forma- Based on numerous ﬁ ndings of ammonites, bivalves, brachio- tion above an unconformity that is shown by erosion, and basal pods, and crinoids, the age of the Desh Formation is reliably conglomerate beds in some places, and records a minor hiatus. 8 Kirillova et al.

Siltstone of the Sinkal’ta Formation is widespread along the east- The thickness of the upper Epikan formation is 900 m. The ern margin of the basin. However, facies changes indicate vari- age is based on the following faunal ﬁ ndings along the Soloni able conditions in some sectors. River: Lissoceras cf. psilodiscus (Schloenb.), Partschiceras gros- Sections of this formation containing fossils were scrutinized sicostatum (Imlay), and Mytiloceramus kystatymensis (Kosch.), along the Soloni River, the BAM track, and the Bureya River by corresponding to the late Bajocian of the Middle Jurassic (Sei et I.I. Sei, E.D. Kalacheva, and D.F. Fomin (Anoikin, 2004; Sei and al., 2004).

Kalacheva, 1980). In the northeastern part of the Bureya Basin, The El’ga Formation (J2el), the most widespread unit in the formation is mainly composed of arkose and graywacke the Bureya Basin, overlies the Epikan Formation conformably (calcareous in some places) sandstone with mytilocerams, bel- or with local variable-scale erosion. In the west, it discordantly emnites, and plant detritus. In the central part of the Gudzhik overlies the rocks of the basement. The thickness of conglomer- trough and the southeastern part of the Bureya trough, its basal ate beds in this formation is as much as 200 m in some places. units incorporate arkose and graywacke sandstone with lenses Erosion, conglomerate, and the marked change of the faunal of gravelstone and conglomerate interbedded with siltstone lay- complexes suggest the existence of a hiatus and perhaps the pres- ers. Above the basal strata, there are dark-gray and greenish-gray ence of an angular unconformity (Sei and Kalacheva, 1980). fi ne-grained sandstone with layers and lenses of siltstone, con- In the northern part of the Bureya Basin, the most complete taining coalifi ed plant detritus in some places, as well as felsic section of the El’ga Formation with well-preserved fauna crops lava and ashes. In some places, intercalated dark-gray graywacke out along the Bureya and Umal’ta Rivers (Sei and Kalacheva, sandstone and pale-gray medium arkosic sandstone crop out. In 1980). Here, the undifferentiated El’ga Formation is mainly the upper portion of the sequence, fi ne sandstone beds contain composed of fi ne arkosic and polymictic sandstone with lay- marcasite pellets. The thickness of the formation in the Dublikan ers of medium-grained silty sandstone, siltstone, and mudstone Basin is ~750 m. Based on the numerous remains of ammonites, that contain numerous inclusions of coalifi ed wood and marca- mytilocerams, gastropods, and belemnites, the age of the forma- site concretions in some places. The base of the section includes tion is estimated as the Aalenian–early Bajocian (Anoikin, 2004; sandstone with small pebbles and lenses of small-pebble con- Sei and Kalacheva, 1980; Sei et al., 2004). glomerate, whereas the top of the section includes intercalated

The Epikan Formation (J2ep) overlies the Sinkal’ta For- ﬂ yschoid sandstone and siltstone. The thickness of the formation mation conformably or with conglomerate at the bottom. This is as much as 1800 m (Sei and Kalacheva, 1980). formation is marked by the prevalence of siltstone at the basin In the Urgal–Chegdomyn interﬂ uve area, the formation, center (the Soloni River area), the greenish and dark-green (up ~2200 m thick, is represented by alternating beds of sandstone to black) color of the rocks, the conchoidal cleavage, and an and siltstone with layers (up to 10 m thick) and lenses of tuffa- abundance of marcasite concretions. Based on the lithology and ceous siltstone, gravelstone, conglomerate, lava, and tuff (Anoi- organic remains, the Epikan Formation is divided into lower and kin, 2004). The sandstone commonly includes arkose and gray- upper parts, which are reliably recognized north of the Chegdo- wacke, as well as tuffaceous and calcareous beds. Unfortunately, myn River. In some sectors, e.g., between the Malaya El’ga and the fauna in this section is scanty. Based on the lithology, the Chegdomyn Rivers, each part may further be divided into mem- El’ga Formation in this section is divided into subformations, bers in which the lower beds are dominated by sandy material which are further subdivided into members that emphasize the and the upper ones by siltstone and mudstone. The lower Epikan cyclic structure of the formation.

(J2ep1) is mainly composed of siltstone, which is sandy in some In the Soloni–Dublikan interfl uve area (the central part of places. At other localities, arkosic sandstone and graywacke, the basin), the basal portion of the section (218 m) has a fi ner- tuffaceous siltstone, rhyolite fl ows and breccia, and mudstone are grained composition. It is represented by clayey sandstone and also included. The thickest, up to 900 m thick, section of this siltstone with a diverse faunal complex. This gives way to the subformation was reported from the basins of the Bol’shaya and typical “ammonite” horizon (18 m) with numerous remains of Malaya El’ga Rivers. In the southern section of the subforma- ammonites. This horizon is overlain by a thick member of silt- tion exposed along the Soloni River, the psammite fraction is less stone (Sei and Kalacheva, 1980; Sei et al., 2004). common, and the thickness is reduced to 700 m. Faunal remains In the southern part of the Bureya trough, left bank of the in the lower subformation are early Bajocian (Anoikin, 2004; Sei Dublikan River, Adnikan River basin and Gudzhik trough, the et al., 2004). bottom of the El’ga Formation includes 40–300 m of conglom-

The upper Epikan (J2ep2) is most completely exposed and erate, gravelstone, and coarse-grained arkosic sandstone. The well studied in the Soloni River section, where it is composed of overlying unit is composed of intercalated thin-bedded, mainly homogeneous, thin-bedded siltstone with marcasite concretions ﬁ ne-grained sandstone and siltstone. The section also includes up and lenticles of sandstone and mudstone. The base of the unit to 50-m-thick members of the intercalated sandstone, siltstone, may contain a horizon of ﬁ ne- to coarse-grained sandstone that and mudstone (up to 15 cm thick). The thickness of the forma- gradually overlies the siltstone of the lower subformation. In the tion in this area is as much as 1050 m (Anoikin, 2004). The El’ga basin of the Bol’shaya and Malaya El’ga Rivers, the upper sub- Formation includes numerous and diverse remains of fossil fauna formation is divided into sandstone and siltstone members. mainly represented by ammonites and bivalves that are typical Geodynamic evolution of the East Asian continental margin in the Mesozoic 9

of the late Bajocian–Bathonian (Sei and Kalacheva, 1980; Sei et SEQUENCE STRATIGRAPHIC MODEL OF al., 2004). THE BASIN

The Chagany Formation (J2g) is confi ned to the Bureya trough, where lower and upper parts are recognized. The lower The Mesozoic section and unconformities may be inter- part represents an alternation of graywacke, sandstone, and silt- preted to construct a sequence stratigraphic model (Fig. 6). stone with tuffaceous siltstone layers (400 m in total). The upper Interpreted events may be correlated with geological processes, part is dominated by siltstone with rare beds and layers of gray- such as tectonics, eustasy, volcanism, and stages of biota change, wacke, mudstone, and tuffaceous siltstone (also 400 m in total). which affected the accumulation of the rock units. The bottom of the upper part includes a horizon of sedimentary Unconformity-bounded stratigraphic sequences in the breccia (5–8 m thick). Bureya Basin are correlative with the latest Indo-Sinian (Late In the western part of the trough, the formation discordantly Triassic) and Yanshanian (Jurassic–Early Cretaceous) second- overlies the basement represented by Paleozoic granites or rocks order cycles according to the Asian scale (Ren et al., 1999) or of the El’ga Formation (Markov et al., 1970). In all the sections Kimmerian cycle from the European scale (Graciansky et al., studied, the bottom includes 20–50 m of fi ne sandstone or con- 1998). The Indo-Sinian cycle in the Bureya Basin is represented glomerate. Overlying, distinct gray, siltstone beds include sev- only by a Late Indo-Sinian subcycle of the Late Triassic–age eral interbeds of fi ne-grained, silty arkosic sandstone and gray- third-order cycle or megasequence 1. The Yanshanian cycle is wacke as well as layers of tuffaceous siltstone, mudstone, and subclassifi ed into Early, Middle, and Late Yanshanian subcy- sedimentary breccia (0.1–10 m). Some parts of the section include cles (Ren et al., 1999), which should be regarded as third-order rounded and pillow-shaped marcasite concretions. The upper cycles (Fig. 6). part of the section accommodates similar concretions of calcare- The boundary between Early and Middle Yanshanian sub- ous siltstone. The beds commonly contain coalifi ed plant detritus. cycles, ca. 150 Ma, is marked by a succession of geological The thickness of the formation changes from 530 m to 1000 m events. These involve the fi rst episode of early Yanshanian (Sei and Kalacheva, 1980). The faunal remains commonly found in orogeny, recorded by the middle Kimmerian unconformity, the upper portion of the section include ammonites, mytilocerams, between ca. 179 and 175 Ma, concurrent with the late Toar- and small bivalves (Markov et al., 1970; Sei and Kalacheva, 1980; cian regression and a short-term warming (moderate sub- Sei et al., 2004). According to E.P. Brudnitskaya (1980, personal tropical climate, according to V.A. Vakhrameev [1988, per- commun.), the remains of belemnites, Meleagrinella, and Pleuroy- sonal commun.]), followed by a rapid cooling in the Middle meia are present, although the exact sample locations in the forma- Jurassic. At the middle-late Yanshanian cycle boundary in the tion remain unclear. The age of the formation is estimated as late limits of the territory under study, the second episode of the Bathonian (Sei and Kalacheva, 1980; Sei et al., 2004). early Yanshanian orogeny and the fi rst episode of the middle Yanshanian orogeny agree very closely (Ren et al., 1999), as Middle–Upper Jurassic (Callovian to Oxfordian) refl ected in a long-term late Oxfordian–Kimmeridgian break in sedimentation. Within the early to middle Yanshanian cycles,

The Talyndzhan Formation (J2–3 tl) marks the onset of coalif- two activation episodes have been recognized that are marked erous continental sedimentation in the Bureya Basin. In the cen- by unconformities. The fi rst episode happened 180 m.y. ago, tral part of the Bureya trough, the rocks disconformably overlie while the second one lasted in the range of 170–150 Ma (Ren horizons of the Chagany and El’ga Formations above a surface et al., 1999). In the limits of the middle Yanshanian cycle, a of erosion. In the western part, they nonconformably rest upon large orogenic event—collision between the Siberian and Paleozoic granitoids of the Bureya Massif basement. The Tal- Sino-Korean cratons—occurred in the Far East of Russia that yndzhan Formation may be divided into upper and lower parts commenced in the west in Transbaikalie in the latest Triassic (Turbin, 1994), which further may be subdivided into members and terminated in Priokhotie in the Middle Jurassic (Kirillova, emphasizing the cyclic structure of the section. 2003) and resulted in amalgamation of the terranes and blocks In most of the sections studied, the lower portion of the for- into a single Asian craton. The earlier dominant nearly latitu- mation is composed of 100–200 m of fi ne- and medium-grained dinal (Tethyan) structure orientation was replaced with nearly arkosic sandstone with common inclusions of the coalifi ed plant meridional (Pacifi c) structure orientation. The Late Jurassic remains. The upper part consists of as much as 330 m of silt- is considered to mark the onset of riftogenesis in East Asia stone, sandstone, tuffi te, mudstone, and tuff with spacing of 4 to (Kirillova, 2008; Ren et al., 1999), accompanied by volcanic 50 m. The siltstone–tuffi te–mudstone strata include coal layers activity and warming, as is testifi ed by the composition of the and seams ~5.75 m thick. The thickness of the formation ranges richest Late Jurassic fl ora in the Bureya Basin. In the Bureya from 360 to 480 m. The section is represented by abundant plant Basin at this time, N-E–striking displacements also activated, remains: Raphaelia diamensis Sew., Coniopteris burejensis (Zal.) along which the Kyndal graben began to form. Sew., Cladophlebis aldanensis Vachr., Nilssonia schmidtii (Heer) Thus, considering the time of manifestation of global, sub- Sew., Sphenobaieria umaltensis Krassil., and others. This fl ora global, and regional events in eastern Asia, six megasequences complex suggests a Callovian–Oxfordian age (Turbin, 1994). (third-order cycles) are distinguished in the Late Triassic to 10 Kirillova et al. Sub- Cycles s Age, Orogeny and taphrogeny Mega- Sedimentation stage Formations/sequences sequence, Sequences Stage Ma first- second- third- (fifth-order cycles) Rate, m/Ma SERIES and their thickness, m (Ren et al., 1999) order Facie SYSTEM order order MS P L Danian S 6.1 – 10 Ma 30 65.5 Sandstone strata, Maastrichtian, U 300

Km2

L 70.6 , 6 Campanian, U M Kkm 2 L 83.5 l -K s U 21

Santonian, 12 M 30 Ma, Kst Ks 2 L 85.8 Upper Megasequence - U continenta

Coniacian, Himalayan M Kk 2 L 89.3 Turonian, U M Kt2 L 93.5 U Cenomanian, M ,

Late Yanshanian 5 Ks 2 L 99.6 S 5.2 – 10.2 Ma Kyndal Fm., K1-2 kn, 74-88 U 750-1050 2 Albian, M Sikhote-Alin 21

Kal1 a-Ks

1 S 5.1 – 9.8 Ma 20 Ma,

L Iorek Fm., K ir, K 112.0 1 56-71 550-700

U Megasequence - Aptian, Middle Yanshanian Ka1 2nd episode S 4.3 – 9.3 Ma L 54-65 125.0 Chemchukin Fm., K1 m, 500-600 CRETACEOUS U Barremian, S 4.2 – 8.9 Ma kbr L 1 130.0 11-67 Chegdomyn Fm., K1 g,

Lower Hauterivian, U 100-600

Kh 1 1 L 136.4 Ma, Late Yanshanian subcycle Late Yanshanian

Valanginian, U tt - K a S 4.1 – 14.4 Ma 3 1 Solony Fm, K1 sn, 32 Kv J 1 L 600

140.2 l J31 tt - K v 60-83 Berriasian, U Megasequence - 4, M Kb1 L 145.5 31 J-Kur

U continenta Tithonian, Urgal series, Jtt M Dublikan Fm, J3 db, 3 250–600 L 150.8 Middle Yanshanian Kimmeridgian, U 1st episode

Jkm3 L 155.7 U Upper Oxfordian, M Early Yanshanian Jo3 2nd episode L 161.2 Late Kimmerian Yanshanian LPIAN U unconformity Talyndzhan Fm, J2-3 tl, 250–600 Callovian, A S 3.3 – 7.4 Ma M Jbt2 - Jo Jc2 23 140-190

L 164.7 km U Chagany Fm, J g, 800–1000 Bathonian, 2 subcycle Yanshanian a - J 25 Ma

M 2 3

Jbt2 J L S 3.2 – 3.5 Ma

167.7 Elg'a Fm, J el, 1000–2200 Megasequence - 3, 2 22 70-630 J b - J bt Middle 22 Bajocian, U

Middle Collision of the Siberian Epikan Fm, J ep, 900–1400 Jb 2 and Sino-Korean cratons along the 2 L 171.6 Mongol–Okhotsk suture S 3.1 – 5.5 Ma 2 127-180 Ja22 - Jb Aalenian, U Sinkal'ta Fm, J2 sn, 700–1000

Ja2

JURASSIC L 175.6

Toarcian, U Early Yanshanian

Jt marine 1 L 1st episode S 2.2 – 5 Ma 183.0 21 Desh Fm, J1dš, 400–700 Middle Kimmerian unconformity 80-140 Jp11 - Jt 2 -t s

Pliensbachian, U 1 J 18 Ma Yanshanian Yanshanian

Jp subcycle 1 L 189.6 Lower Megasequence - 2, Early Taksa Sequence, J1 tk, 600–1000 S 2.1 – 3.5 Ma 2 500-630 Sinemurian, U Js Khavagda Sequence, J1 hv, 1250 1 Js1 L 196.5 Hettangian, 1

Jg1 199.6 Rhaetian, 3 1 T-Js Tr 23 Ma 3 203.6 Late Indo-Sinian Early Kimmerian subcycle Norian, Demkukan Sequence, T3 d S 1.1 – 3.4 Ma 3 118 Upper Megasequence - 1, 3 U Late Indo-Sinian unconformity Tn3

400 Indo-Sinian TRIASSIC Tn3 207.0

Figure 6. Sequence stratigraphic and cycle model for the Bureya Basin. Geodynamic evolution of the East Asian continental margin in the Mesozoic 11

Cretaceous succession, being in turn subdivided into sequences Formation occurs conformably on the Taksa Formation (Anoikin, (fourth-order cycles). The sequences are also rhythmically com- 2004). In the latest Early Jurassic (late Pliensbachian–Toarcian), posed and experience natural facial variability along and across the Izanagi plate continued to subduct, and fragments of the accre- the basin. However, the uniform lithology, at random faunal tionary complex were involved in the giant delta fans on the con- occurrences, hampers the determination and correlation of fi fth- tinental margin. Thick late Pliensbachian transgression, although and sixth-orders cycles, so that they are identifi ed reliably only in not global, was manifest clearly in the Far East. The sea penetrated sequence 3.2 (Elga Formation), in which discrete horizons have into eastern Transbaikalie along the Mongol-Okhotsk suture. been well correlated owing to the abundance of faunal fi ndings The north-northeastern orientation of the Bureya Basin, sup- (Kirillova and Krapiventseva, 2012). ported by gravity data and the parallel strike of the Tastakh system of faults, suggests that the continental margin during the Jurassic STAGES OF THE GEODYNAMIC EVOLUTION had the same orientation. By that time, the Amgun block, composed of Permian to Triassic sediments, was likely lowland and The geodynamic evolution of the Bureya Basin is closely defi ned the eastern boundary of the Bureya paleobasin. Changes related with both global and regional events (Kirillova, of the marine environment to continental and shifting of the basin 2003, 2008). The general structure of the basin is shown in a boundary westward are shown in Figure 9. During the Desh time lithological-facies profi le (Figs. 7, 8). According to the recon- (late Pliensbachian–early Toarcian), its depocenter was located structions (Maruyama et al., 1997; Ren et al., 1999), collision near the eastern edge. between the Yangtze and Sino-Korean blocks was terminated by The sediments of the Sinkal’ta and Epikan Formations were the Indo-Sinian orogeny in the Middle Triassic. deposited in the same geodynamic setting. The sedimentation Following tectonic exhumation of the high-compression met- rate ranged from 80 to 180 m/m.y. The fi rst episode of the Yan- amorphic rocks, intense uplift, and erosion along the Qinling-Dabe shanian movements occurred in the Early Jurassic (Ren et al., suture, eroded material was transported northeastward forming a 1999) and was expressed in the late Toarcian break in sedimenta- vast delta. The Norian transgression facilitated this process. The tion (Fig. 6). Termination of the collision between the Jiamusi- Bureya Basin was the depositional center of sequence 1.1, depos- Bureya and Siberian cratons along the Mongol-Okhotsk and Jilin ited along its margins as rudaceous rock units (Mereksky and sublatitudinal sutures took place in the Middle Jurassic. As a Demkukan rock units, Late Triassic). Concurrently in the Late Tri- result, the North Asian, Sino-Korean, and Yangtze cratons, along assic, the slow frontal subduction of the mid-oceanic ridge (MOR) with the orogenic belts separating them, combined to form a sin- between the Izanagi and Farallon plates beneath the Asian margin gle NNE-oriented Eurasian plate. The Izanagi plate orthogonally with a rate of 4.7 cm/yr took place approximately at the latitude subducted beneath the Eurasian plate at a rate of 4.7 m/m.y. from of the southern Primorye (42°N). The Mino-Tamba-Chichibu- the east (Maruyama et al., 1997) forming a subduction complex Nadanhada-Samarka accretionary complex was formed in the on the continental margin that extended from Chukotka to Philip- frontal part of the continental margin. The complex, along with pine Islands. the plate, which continued to move, exerted compression on the Global tectonic processes were expressed in the Bureya continental margin, leading to its uplifting and break in sedimen- Basin. Most likely, compression, elevation, and rapid disrup- tation during the Rhaetian through Sinemurian. According to the tion (the rate of sedimentation attained 630 m/m.y.) caused the available reconstructions (Maruyama et al., 1997), the passive con- displacement of the sedimentary depocenter. In addition, the tinental margin at that time extended in the meridional direction. structural character of the basin changed as the deposits of the At the beginning of the Early Jurassic, the character of the Elga Formation with a thick conglomerate bed (~200 m) and azi- plate convergence in the east remained almost unchanged. In east- muthal unconformity occur at different horizons of the underly- ern Transbaikalie, scissor-like collision between the Sino-Korean ing sediments. As a consequence of the continued transgression, and Siberian blocks started in the west along the Mongol-Okhotsk they became more widely distributed compared to all the under- suture in the Early Jurassic and was slowly shifted eastward. lying formations. These events were most likely due to reorganization of lithosphere Late Bathonian–Callovian deposits of the Chagany and Tal- plate movements (Maruyama et al., 1997). As a result, the volumi- yndzhan Formations accumulated in the conditions of the shoal- nous terrigenous clastic material was removed eastward along the ing marine basin. During Talyndzhan time, marine sedimenta- suture to form a huge delta in the frontal part. The clastic material tion was replaced by continental sedimentation. A long-term late spread over the continental margin and formed thick sedimentary Oxfordian–Kimmeridgian break is recorded throughout sizable complexes in the marginal continental basins including the Uda, territories of the overall Bureya Basin and adjacent regions east- Torom, Bureya, and western Sanjiang-Middle Amur basins. Dur- ward. The late Kimmeridgian unconformity can probably be ing the late Sinemurian, 2000-m-thick sediments accumulated in attributed to a manifestation of the fi rst episode of the early Yan- the Bureya Basin (Khavagda, Taksa series). The rate of sedimen- shanian and the fi rst episode of the mid-Yanshanian movements tation was very fast, reaching 500–630 m/m.y. in East Asia (Ren et al., 1999). The early Pliensbachian hiatus (Fig. 6) was not long and The Tithonian was the time of activation of various tec- universally expressed, because in the Gudzhik trough, the Desh tonic processes. At that time, the rate of oblique subduction in 12 Kirillova et al. + /s /s 3 + 3 + + SE 98 t 55 t + 1A 3200 m + + + + 2 + + -2.46-2.48 MK -2.54-2.61 1 -2.29 -7.8-8.1 1 -2.51-2.56

-4.5-6.2 -15.7 -2.5-6.6 1 ρ 1 δ

δ ρ δ p ρ ρ δ -2.33-2.43 2

-9.8-13.2 1

δ ρ -MK 34 -MK 23 -MK 23 Q+K gas-water manifestation Siltstones: Siltstones: Siltstones: 2 Siltstones: MK fault ? ur break in sedimentation m g kn gas logging oil films ir en, Bureya Basin, from deep boreholes. en, Bureya 1 1 1 1-2 31 m-310 K K K K J-K m-398 m-437 m-581 m-890 ? m-382 3 MK 34 MK -MK 2 -2.63-2.64 23 1 -2.60-2.65 1 ρ ρ MK -2.38-2.45 MK -MK ? 1 ρ -2.37-2.61 1 tl ρ 2-3 J coal + coaly mudstone - 43 m (7%) g m sn kn 1 ir 1 1 1-2 coal + coaly mudstone-80 m (14%) 1 K m-608 m>569 3 K K K K m-440 2890 m-730 m-513 m-429 Jdb m-170 1C 3459 m 2 p 2 MK 1 2 2 2 -12-14.7 -2.23-2.54 -2.14-2.19 -15.5-17.8 -2.38 -12.8 Q+K 1 2-3 1 1 1 1 1 -2.44-2.51 -4.6-8 -2.44 1 δ -3.6 ρ 1 MK ρ δ ρ MK MK δ 2 1 MK 1 ρ δ ρ δ MK -10.7 -2.38 1 1 MK δ ρ 3 3 g m kn 614 ir - 1 1 1 1-2 m>442 K m K K K m-534 m-402 m-845 500 m /d 500 m /d x) m-175 saturation porosity, % saturation porosity, 3012 m - ; δ ? tl 3 3 3 2-3 m J m>98 kn ir 1-2 1 g/c m-30

200 m /d K m-610 m-476 m-488 K m-876 200 m /d m-524 = = = 3102 m density total porosity, % total porosity, - -; -; 1 1 ρ x) degassing of drilling mud, oil films δ ) tl 2-3 sn ? J m>61 + db ( ur g m kn 1 ir 31 1 1 1-2 m-505 K J-K m-486 K K m-642 m-524 K m-783 Catagenetic gradients are given from porosity and density Figure 7. Scheme of the formation and section correlations, rock catagenesis, and oil-and-gas manifestations in the Kyndal grab Figure 7. Scheme of the formation and section correlations, rock catagenesis, oil-and-gas manifestations in Kyndal 3006 m NW 400 800 200 600 3200 1000 1200 2000 2200 2800 2400 2600 3000 3400 1400 1600 1800 Geodynamic evolution of the East Asian continental margin in the Mesozoic 13

Figure 8. Lithological-facies proﬁ le of Jurassic–Lower Cretaceous sediments ﬁ ll- ing the Bureya Basin. 1—conglomerate, 2— sandstone, 3—siltstone, 4—coal, 5—acid volcanics, 6—Proterozoic underlying meta- morphic rocks (PR), 7—late Paleozoic granitoids, 8—fault.

the east sharply increased, reaching ~30.0 cm/yr, and its direc- and coarse-grained sandstone at the base of the Aptian to early tion changed into a meridional one (Maruyama et al., 1997). As Albian Iorek Formation. a result, a transform continental margin was produced, along Final geologic processes recorded by strata in the Bureya which an accretionary prism and a series of thrusts continued to Basin formations are related to the late Yanshanian orogeny (Ren form. At the same time, active rifting commenced in the Eurasian et al., 1999). It combined different processes that took place continent, which was expressed in (1) intense volcanic activity during the Albian through early Cenomanian. In the Albian, the (the Lesser Khingan volcanic belt with 1000 m thick volcanites), oblique subduction of the Izanagi plate went on, and compres- (2) formation of a vast province of “basins and ridges” (~300 sion processes were prevalent at the continental margin. Collision grabens and half grabens), and (3) formation of transtensional in southeastern Russia spread laterally eastward and northward; basins along large NE left-lateral strike-slip faults of the Tan-Lu therefore, folding and emplacement of collision-related granites system (Kirillova, 2008). These processes were marked in the generally are dated at the middle Albian–early Cenomanian. eastern margin of the Bureya Massif as NE-oriented faults (Mel- The major Sikhote-Alin folding, related to accretion, took ginsky and Khingan; Fig. 1) and the Kyndal graben bounded by place in the early Albian. Afterward, terrigenous and volcano- the Urgal and Kyndal faults. The depocenter of sedimentation genic molasse accumulated. In the Bureya Basin, the Sikhote- was displaced to the west (Fig. 8). Rifting is attested by the depth Alin orogeny led to relief renewal and intense erosion. Uplift is of the Moho discontinuity beneath the graben. recorded by the erosion at the base of the Kyndal Formation and During the Aptian, the oblique subduction of the Izanagi acceleration of sedimentation rate, which is estimated to have plate continued with a rate of 20.7 m/m.y. (Maruyama et al., been as high as 138 m/m.y. 1997). Intense volcanic activity took place in the western In the middle Albian to Cenomanian, the oblique subduc- Pacifi c and adjacent continental margin. The regional data tes- tion of the Izanagi plate continued, resulting in activation of the tify that the regime of a transform margin setting with a sub- strike-slip faults of the Tan-Lu system. Small troughs fi lled with stantial transtensional component also remained in the Aptian coarse-grained volcanogenic-sedimentary sediments of the Lak- in the study territory. In particular, small, nearly longitudinal sky series, ~600 m thick, were formed along the Khingan fault near-fault grabens fi lled with tuffs and alkali basalt lavas, and and a series of other faults in the eastern part of the Bureya Basin terrigenous sediments containing Aptian to Albian fl ora were (Vas’kin et al., 2009). The Kyndal Formation within the Kyndal deposited in the easterly areas of the Bureya Basin (Vas’kin et graben has a northeastern direction. al., 2009). As a result of ascending movements, the third mem- Contraction in the east resulted in the formation of thrust ber of the Chegdomyn Formation (300 m) became eroded in faults along the eastern margin of the Bureya Basin. The thrust the mid-Aptian, followed by the formation of the Kyndal and faults probably formed in response to the collision and pressure of Urgal faults caused by riftogenic processes. This marked the the Okhotsk plate. By the end of the Albian, small intrusions of the transformation of the Kyndal synsedimentation fold into a Iorokhan complex were emplaced, often having a ribbon form and graben-syncline (Fig. 9). According to Ren et al. (1999), in the a nearly longitudinal strike. Intense Late Cretaceous volcanic pro- middle Aptian (120 Ma), the second episode of the middle Yan- cesses occurring at the eastern margin of the continent were mani- shanian orogeny happened in northeastern Asia. Other than the fest in the Bureya Basin by the emplacement of small intrusions volcanic activity, and evident renewal of relief, development of and dikes of the Butakan-Churkin and Badzhal-Dusse-Alin com- mountain rivers must have taken place that led to formation of plexes. Abundant submeridionally oriented dikes are particularly boulder conglomerate with gritstone lenses 140–200 m thick common in the Urgal-Chegdomyn interfl uve (Anoikin, 2003). horizontal 1:400 000 14 Scales: Kirillova et al. vertical 1:200 000

Jd1 š

Jtk+hv1

Tdm3 Late Triassic- Early Jurassic

Jep21

Jsn2

Jd1 š

Jtk+hv1

Tdm3 Bajocian Aalenian-Early

Jel2

Jep2

Jsn2

Jd1 š for unit abbreviations. Bathonian Jtk+hv1

Tdm3 Late Bajocian-Middle

Jg2

Jel2 Jep2

Jep2 Jsn2

Jsn2 Jd1 š Marine sedimentogenesis Marine Bathonian Jd1 š Jtk+hv1 Middle/Late

Jtk+hv1

Tdm3 Tdm3

Jtl2-3 Jel2 Jep2

Jg2 Jel2 Jsn Jel 2 2 ep Jd1 š Jep2 Jsn2

Jd1 š J1 tk+hv Jsn2

Jd1 š Jtk+hv1 Oxfordian Jtk+hv1 Tdm3 Callovian-Early

Tdm3

LATE OXFORDIAN - KIMMERIDGIAN - BREAK IN SEDIMENTATION

J31 db+K sn Jep2 Jg 2 Jel 2 Jsn2 Jd1 š Jtl2-3 Jep2 Jel2 Jtk+hv1

Jsn2 Jep2 dm T 3

š Volgian- J1d Jsn2 Valanginian

Jd1 š Tdm3

Jtk+hv1

Tdm3 lacustrine-valley Continental alluvial- sedimentogenesis Jel2

Jg2 Jsn2 Km Kg1 1 Jd1 š Jtl Jep 2-3 Jel2 2 tk+hv Jg J 1 2 Jsn Jep 2 Jel 2 2 Jdš Tdm Jsn 1 3 Jep 2 v 2 tk+h Jsn J 1 2 Jd1 š Aptian Jd1 š Jtk+hv1

tk+hv Tdm3 Hauterivian-Early

Jg Jtl3 2 Km1 Kir1 Kg1 Jd1 š Kg1

Kir1 Kir 1 tk+hv Jsn2 J 1 Jel Km1 Jg2 2 Jel Km1 J-Kur31 2 dm T 3 Jd1 š J-Kur31 Jel2 Jep2 Jep2 hv Jtl2-3 tk+ J-Kur31 J 1 Jel Jsn2 Jel 2 Jep2 Jsn2 2 Jtl2-3 Jg2 Jsn2 Jel2 Jd1 š Jd1 š Jep2 Jdš Jtk+hv 1 1 Tdm3 Albian Aptian-Early

Jtk+hv1 Late sedimentogenesis J-Kur31 Jg2

Paralic coastal-marine Kkn Kg1 Kir1 1-2 Kkn1-2 Kir Kkn Km 1 1-2 1 Jg2 V Jel Jel2 Jd1 š Km L 2 1 Kir Kg1 Kir 1 Jtl2-3 1 J-Kur31 J -K Jel2 Jep2 Jep2 31ur Jg2 V Km Jtl2-3 1 L Jsn Kg1 Jg2 Jsn2 2 Jep2 sn J-Kur Jel2 Jel2 31 el Jsn2 Jtl2-3 Jd1 š Jdš Jel2 Jg2 Jel 1 2 Jd1 š J tk+hv Tdm3 V 1 Jep2 L Jtk+hv1 Jel2 Jtk+hv1 Albian-Early Cenomanian γξ Kum1 Kg 1 J-Kur K1 g Km1 Jtl2-3 Km1 K-P21 31 J-Kur31 K1kn Jg2 Jel kn V 2 Jel2 Jsn J ur L 2 Jtl 2- tl 2-3 Kir1 Kkn1-2 3 tl tl Jep ir tl g 2 and Khanchuk, 2012). See Figure 2 A1-A2 (Kirillova along the line Basin evolution scheme of the Bureya Figure 9. Paleotectonic Jel Jep2 g Jg2 2 sedimentogenesis Jtl2-3 Jel Jsn2 Jd1 š K1 m 2 V Kir1 Jep2 L Jsn2 ur Jel2 Kg1 Jel2 Jd1 š Alluvial-lacustrine-valley Km1 Jtk+hv1 Kg1 Jtl Jd1 š J tk+h Jd1 š J-Kur31 2-3 1

J-Kur Jsn V v Tdm3 Danian 31 Jg Jep2 2 Jtl2-3 2 L Jtk+hv1 Jtl2-3 Jel2

Jel2 Maastrichtian- Jg2 Tdm3

- Present boundaries of the Bureya Basin; - Kyndal, U - Urgal faults

- Erosion of the third member K1 m (about 300 m) - Axes of the maximal subsidence compensated by sediments accumulation. Geodynamic evolution of the East Asian continental margin in the Mesozoic 15

Since the Late Cretaceous, uplift has been prevalent, and Dickinson, W.R., 1976, Plate tectonic evolution of sedimentary basins, in Dick- subsidence is recorded only during the Maastrichtian by the for- inson, W.R., and Yarborough, H., eds., Plate Tectonics and Hydrocarbon Accumulation: American Association of Petroleum Geologists, Continu- mation of a sandstone unit. Traces of scattered riftogenesis of ing Education Course Notes Series 1, p. 1–27. the East Asian rift belt are represented by small exposures of the Fischer, A.G., 1975, Origin and growth of basins, in Fischer, A.G., and Judson, Miocene basalts in the Soloni River basin. S., eds., Petroleum and Global Tectonics: Princeton, New Jersey, Princ- eton University Press, 322 p. At present, the territory of the Bureya Basin is characterized Graciansky, P.Ch., Hardenbol, J., Jaquin, T., and Vail, P.R., eds., 1998, Meso- by high seismicity at the intersection of two large lineaments in zoic and Cenozoic Sequence Stratigraphy of European Basins: Society the Gudzhik trough area. The fi rst axis corresponds to faults of of Economic Paleontologists and Mineralogists Special Publication 60, 786 p. the Tastakh system, and the second one to the northeastern Tan- Khanchuk, A.I., ed., 2006, Geodynamics, Magmatism and Metallogeny of East Lu system. The magnitude of the earthquakes is 2.5–5, and the Russia: Vladivostok, Dal’nauka, Book 1, p. 539–552. depth of their depocenters reaches 30 km (Khanchuk, 2006). Kirillova, G.L., 2003, Late Mesozoic–Cenozoic sedimentary basins of active continental margin of southeastern Russia: Paleogeography, tectonics, and coal-oil-gas presence: Marine and Petroleum Geology, v. 20, no. 3–4, CONCLUSION p. 385–397, doi:10.1016/S0264-8172(03)00046-1. Kirillova, G.L., 2008, Etapy pozdnemezozoiskogo-kainozoiskogo riftoobra- zovaniya na yugo-vostoke Rossii i v prilegayushchikh raionakh v svyazi We used the latest geological and geophysical data combined s problemami neftegazonosnosti Dal’nego Vostoka (Stages of the late with earlier geologic studies from the Bureya Basin to develop a Mesozoic and Cenozoic rifting in the southeast of Russia and adjacent comprehensive description of the sedimentary basin and to trace regions in the context of the petroleum problems Far East): Doklady Rus- siikoi Akademii Nauk, v. 419, no. 1, p. 104–107 [in Russian]. its geologic evolution. The tectonic and geodynamic evolution Kirillova, G.L., and Khanchuk, A.I., eds., 2012, Bureya Sedimentary Basin: of the Bureya Basin has been analyzed in the context of present- Geological-Geophysical Characteristics, Geodynamics, Fuel-Energy day approaches. The basin is interpreted as a compound hybrid- Resources. Book 4: Vladivostok, Dalnauka, 360 p. [in Russian]. Kirillova, G.L., and Krapiventseva, V.V., 2012, Mezotsiklichnost’ type basin that underwent several evolution stages resulting in verkhnetriasovo-yurskikh otlozheniy Bureinskogo basseina: Tektonika, a change of the structural character. During the Late Triassic to evstatika, sekvensstratigraphiya (Mesozoic cyclicity of Upper Triassic to Middle Jurassic, the basin was formed on the passive continen- Jurassic deposits of the Bureya Basin: Tectonics, eustatics, and sequence stratigraphy, the Far East): Tikhookeanskaya Geologiya, v. 31, no. 4, p. tal margin with edge submeridional rifts. The sedimentation was 38–54 [in Russian]. infl uenced by erosion of an active continental margin. During the Markov, V.A., Trofi muk, A.A., and Shcherbakov, V.S., 1970, Relations between Late Jurassic through Cretaceous, it was an intracontinental pull- marine and coaliferous sediments in the Bureya Trough: Doklady Aka- demii Nauk USSR, Seriya Geologicheskaya, v. 191, no. 3, p. 647–649 apart basin trending NE. [in Russian]. Maruyama, S., Isozaki, Y., Kimura, G., and Terabayashi, M., 1997, Paleogeo- ACKNOWLEDGMENTS graphic maps of the Japanese Islands: Plate tectonic synthesis from 750 Ma to the present: The Island Arc, v. 5–6, p. 113–142. Nittrouer, C.A., Austin, J.A., Field, M.E., Kravitz, J.H., Syvitski, J.P.M., and We would like to express our appreciation to T.L. Karpova and Wiberg, P.L., eds., 2007, Continental Margin Sedimentation: From Sedi- L.V. Yakhno, who helped to prepare the drawings. Thanks are ment Transport to Sequence Stratigraphy (Special Publication 37 of the IAS): Malden, Massachusetts, Blackwell Publishing, 549 p. also due to L.D. Peskova, who translated the manuscript into Reinlib, E.L., 1987, Tektonika Bureiskogo Basseina (Tectonics of the Bureya English. The study was supported by the Far Eastern Branch of Basin): Tikhookeanskaya Geologiya, v. 6, p. 78–84 [in Russian]. the Russian Academy of Sciences projects 12-I-П-27-06, 12-II- Ren, J., Wang, Z., Chen, B., Jiang, Ch., Niu, B., Li, J., Xie, G., He, Zh., and Liu, Zh., 1999, Tectonics of China from a Global View—A Guide to the СУ-08-009, and НК12-05-91158/13-GFEN. Tectonic Map of China and Adjacent Regions: Beijing, Geological Pub- lishing House, 32 p. REFERENCES CITED Turbin, M.T., ed., 1994, Resolution of 4th Interdisciplinary Regional Strati- graphic Conference on the Precambrian and Phanerozoic of the Far East and Eastern Transbaikal Region: Khabarovsk, Russia, 124 p. [in Russian]. Allen, P.A., and Allen, J.R., 1990, Basin Analysis: Principles and Applications Sei, I.I., and Kalacheva, E.D., 1980, Melovaya biostratigraphiya nizhne- (1st ed.): London, Blackwell Science Publications, 451 p. sredneyurskikh otlozheniy Dal’nego Vostoka (The Cretaceous Biostrati- Anoikin, V.I., 2003, State Geological Map of the Russian Federation Bureya graphy of the Lower to Middle Jurassic Deposits of the Far East): Lenin- Series Sheet M-53-VIII, Chegdomyn: Saint-Petersburg, VSEGEI, scale grad, Nedra, 186 p. 1:200,000, 123 p. Sei, I.I., Okuneva, T.M., Zonova, T.D., and Kalacheva, E.D., 2004, Atlas mezo- Anoikin, V.I., 2004, State Geological Map of the Russian Federation Bureya zoiskoy morskoy fauny Dalnego Vostoka Rossii (Atlas of the Mesozoic Series Sheet M-53-XIV, Suluk (2nd ed.): Saint-Petersburg, VSEGEI, marine fauna of the Far East, Russia): Saint-Petersburg, VSEGEI Publica- scale 1:200,000, 102 p. tion, 234 p [in Russian]. Bally, A.W., 1975, A geodynamic scenario for hydrocarbon occurrences, in Vas’kin, A.F., Dymovich, V.A., Atrashenko, A.F., et al., 2009, State Geo- Proceedings of the IX World Petroleum Congress, Tokyo, Volume 2. logical Map of the Russian Federation Far Eastern Series Sheet M-53- Geology: Barking, UK, Applied Scientifi c Publishing, p. 33–44. Khabarovsk (3rd ed.): Saint-Petersburg, VSEGEI, scale 1:1,000,000. Bally, A.W., and Snelson, S., 1980, Realms of subsidence, in Miall, A.D., ed., Welte, D.H., Horsfi eld, B., and Baker, D.R., eds., 1997, Petroleum and Basin Facts and Principles of World Petroleum Occurrences: Canadian Society Evolution: Insights from Petroleum Geochemistry, Geology and Basin of Petroleum Geologists Memoir 6, p. 9–75. Modeling: Berlin, Springer-Verlag, 535 p. Busby, C.J., and Ingersoll, R.V., 1995, Tectonics of Sedimentary Basins: Oxford, UK, Blackwell Science Incorporated, 579 p. Dickinson, W.R., ed., 1974, Plate Tectonics and Sedimentation: Society of Eco- MANUSCRIPT ACCEPTED BY THE SOCIETY 3 FEBRUARY 2015 nomic Paleontologists and Mineralogists Special Publication 22, 27 p. MANUSCRIPT PUBLISHED ONLINE 6 NOVEMBER 2015

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