Jurassic–Cretaceous Terrestrial Transition Red Beds in Northern North

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Palaeoworld 26 (2017) 403–422

Jurassic–Cretaceous terrestrial transition red beds in northern

North China and their implication on regional paleogeography,

paleoecology, and tectonic evolution

∗

Huan Xu, Yong-Qing Liu , Hong-Wei Kuang, Yan-Xue Liu, Nan Peng

Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China

Received 21 December 2015; received in revised form 26 April 2016; accepted 19 May 2016

Available online 25 May 2016

Abstract

The Jurassic–Cretaceous terrestrial transition red beds in the northern North China Craton are associated with a number of major geological

issues that remain controversial, such as paleogeography, biotic transition, and tectonic evolution. Based on previous studies and new progress

related to stratigraphy, sedimentology, provenance, biotas, and tectonics, this paper performs a comprehensive review of the red beds in the northern

North China Craton represented by the Tuchengzi/Houcheng/Daqingshan Formation (ca. 154–137 Ma) and offers some new perspectives. Based

on the 15 measured sections, ﬁve facies units including alluvial fan, ﬂuvial, delta, lacustrine, and eolian facies have been recognized and described

in detail. Provenance analysis indicates that the red beds were derived from local sources. Deposits in the basins in the eastern Yinshan–Yanshan

orogenic belt were derived mainly from volcanic rocks of the Middle–Late Jurassic Tiaojishan Formation and the Mesoproterozoic–Early Paleo-

zoic carbonate, siliceous, and clastic rocks present around the basin, especially in the north. In contrast, sediments in the basins in the western

Yinshan–Yanshan orogenic belt were provided predominantly by the Neoarchean–Paleoproterozoic metamorphic rocks exposed mainly in the

north of the basin. Paleocurrent features in different regions show characteristics of a localized convergent paleo-drainage system, suggest-

ing that a series of relatively independent small- to mid-scale basins developed in the northern North China Craton. The east–west-trending

Yinshan–Yanshan orogenic belt, formed in the late Middle Jurassic, uplifted successively and constituted a paleogeographic highland in northern

North China during the Jurassic–Cretaceous transition time. The presence of eolian deposits in the early Early Cretaceous indicates degradation of

the severe arid and hot environment, which may have been an essential factor in the dying out of the Yanliao Biota. Combined with regional Late

Jurassic–Early Cretaceous A-type granites, maﬁc dykes, and metamorphic core complexes and rift basins, this suggests that the Jurassic–Cretaceous

transition red beds were formed in an extensional tectonic setting controlled by the post-orogenic collapse of the Mongol–Okhotsk

orogenic belt.

Keywords: Jurassic–Cretaceous; Tuchengzi/Houcheng/Daqingshan Formation; Transition red beds; North China Craton

1. Introduction been well recorded in marine strata (Handschumacher et al.,

1988; McClelland and Gehrels, 1992; Bertotti et al., 1993;

The breakup of Pangea, the expansions of the Atlantic and Monger et al., 1994; Adatte et al., 1996; Jadoul et al., 1998;

Tethys Oceans, and the subduction of the Paciﬁc Plate caused Hathway, 2000; McDermid et al., 2002; Ellouz et al., 2003; Ford

major impacts on global plate framework, paleogeography, and and Golonka, 2003; Golonka, 2004; Weissert and Erba, 2004;

paleoecology during Late Jurassic–Early Cretaceous (Winterer, Isozaki et al., 2010; Sofonova and Santosh, 2014), but remain

1991; Veevers, 2004). These major geological events have poorly studied in terrestrial strata.

Two important terrestrial biotas developed in Northeast Asia

in late Mesozoic time: the Yanliao Biota (ca. 165–152 Ma) (Y.Q.

∗ Liu et al., 2012a) and the Jehol Biota (ca. 143–120 Ma) (Zhou

Corresponding author. Tel.: +86 10 68995462.

E-mail address: [email protected] (Y.Q. Liu). et al., 2003; Zhou, 2006; Wei et al., 2008). Both biotas include

http://dx.doi.org/10.1016/j.palwor.2016.05.007

404 H. Xu et al. / Palaeoworld 26 (2017) 403–422

a large number of exceptionally well-preserved feathered non- northern Mongolia and Russia, represents the locus of ﬁnal amal-

avian dinosaurs, mammals, pterosaurs, ﬁsh, and insects (Ji et al., gamation of the Siberian Craton with the Mongolia–North China

1998, 2002; Ren, 1998; X. Xu et al., 1999, 2002; Gao and block (Zorin, 1999). To the south, the Qinling–Dabie–Sulu oro-

Shubin, 2003; X.L. Wang et al., 2005; J. Meng et al., 2006; Luo genic belt separates the NCC from the South China Craton

et al., 2007; Hu et al., 2009; Yuan et al., 2013), recording two (Ratschbacher et al., 2003). The Yinshan–Yanshan orogenic

successive terrestrial ecosystems in the age of dinosaur. In the belt (YYOB), related to the Yanshan movement proposed by

lithological succession between the strata that contain Yanliao Weng (1927), is a Mesozoic intracontinental orogenic belt in

and Jehol biotas, there exists a suite of very thick terrestrial red the northern NCC (Fig. 1A).

beds crossing the Jurassic–Cretaceous (J-K) boundary, namely Northern North China evolved into a continental environment

the Tuchengzi/Houcheng/Daqingshan Formation in the northern since Early Triassic and preserved thick and widely distributed

part of North China Craton (NCC). The J-K transition red beds Jurassic–Cretaceous strata (Fig. 1B). In northern Hebei–western

and their contemporary strata are widely distributed in the north- Liaoning, the Jurassic–Cretaceous can be divided into four

eastern part of North China, Northeast China, and East Mongolia volcanic-sedimentary cycles (Fig. 2): the ﬁrst cycle is character-

(Davis et al., 2001; Graham et al., 2001; H. Xu et al., 2011). Due ized by the Early–Middle Jurassic basic–intermediate volcanic

to the paucity of contained fossils, the red beds remain poorly rocks and coal-bearing clastic rocks; the second cycle comprises

studied. the late Middle Jurassic–early Early Cretaceous intermediate-

In recent years, notable progress has been made concerning acid volcanic rocks and coarse clastic rocks; the third cycle

the evolution of terrestrial biota as well as its paleogeographic, consists of the middle Early Cretaceous acid volcanic rocks and

paleoecological, and paleoclimatic settings in the transitional ﬁne-grained clastic rocks, which are absent in western Liao-

period of J-K boundary (Lockley et al., 2006; X.J. Zhao et al., ning; the fourth cycle is composed of the late Early Cretaceous

2006; H. Xu et al., 2011, 2013a; Xing et al., 2012, 2014; J.P. basic-intermediate volcanic rocks and clastic rocks. The Yanliao

Zhang et al., 2012). and Jehol biotas are preserved in the second and third cycles,

The J-K transition red beds have been increasingly recog- respectively. In western Inner Mongolia (Yinshan–Daqingshan

nized as stratigraphically and geologically important for the area), in contrast, volcanic activities were weak and occurred

regional tectonic evolution of northern NCC in the Mesozoic only in the late Early Cretaceous, and the clastic deposits are

(Y. Zhao, 1990; Davis et al., 1998, 2001; He et al., 1998, 1999, thick (Fig. 2). Two regional angular unconformities represent-

2007, 2008; Davis, 2005; Cope et al., 2007; S.F. Liu et al., 2007; ing an intracontinental orogeny (Yanshan movement) are present

H. Xu et al., 2011, 2012, 2013b; J. Liu et al., 2014). However, the in northern North China; one is under the Tiaojishan/Lanqi

basin structural properties of the Jurassic–Cretaceous deposits Formation, and the other is under the Yixian and Lisangou

and regional tectonic background are hotly debated. These con- formations.

troversies include whether the intense products were controlled The J-K transition red beds, represented by the Tuchengzi

by the compression from thrust faults (Davis et al., 1998, 2001; Formation in western Liaoning, the Houcheng Formation in

He et al., 1998; Cope et al., 2007) or by intraplate extension (Ma northern Hebei, and the Daqingshan Formation in western Inner

et al., 2002; Shao et al., 2003; Y.Q. Liu et al., 2015) or the deep Mongolia, are characterized by light purple, purple-red clastic

strike-slip faults in the northern margin of the NCC (Qu et al., rocks with regional stability (Figs. 3 and 4). Large amounts of

2006) or by the back-arc extension resulted from subduction of high-precision isotopic dating data have constrained the age of

the paleo-Paciﬁc plate (H. Xu et al., 2011). Recent studies based the red beds to 154–137 Ma (H. Xu et al., 2012, 2014) (Fig. 4).

on metamorphic core complexes (MCC), maﬁc dykes, volcanic The J-K transition red beds are widespread in northern North

rocks, A-type granites and rift basins in NCC and Northeast China, with thickness of 800–4000 m (Figs. 1C and 4). In gen-

Asia indicate that large-scale extension may have been initiated eral, they consist of thick-bedded or massive conglomerate in

in the Late Jurassic (S. Liu et al., 2008; Ying et al., 2010; T. Wang the lowermost part, medium–thick-bedded sandstone, siltstone,

et al., 2012; Charles et al., 2013; W.L. Xu et al., 2013; Qi et al., mudstone, and limestone interbedded with conglomerate and

2015). Based on these new results and a more detailed analysis tuff in the lower–middle part, and thick-bedded conglomer-

of the depositional environment and sediment provenance on the ate and cross-bedded sandstone interbedded with tuff in the

J-K transition red beds, this paper comprehensively reviews the middle–upper part in an ascending order (Fig. 3). Tuffaceous

geological issues, such as paleogeographic, paleoenvironmen- or volcanic interlayer is absent in the Daqingshan Forma-

tal, paleoecological, paleoclimatic and tectonic settings in the tion in Yinshan–Daqingshan. The J-K transition red beds have

transitional period of J-K boundary in the northern NCC. conformable or unconformable contacts with the underlying

Tiaojishan (intermediate volcanic rocks, volcaniclastic rocks,

2. Geological background ca. 165–152 Ma) or Changhangou Formation and the overlying

Zhangjiakou (acid volcanic lava and volcaniclastic rocks, ca.

The study area is located at northern margin of the NCC, 143–130 Ma) or Lisangou Formation (Fig. 3).

which is bounded by the Late Paleozoic–Early Mesozoic oro- Although the fossils preserved in the J-K transition red beds

genic belts both to the south and to the north. To the north, the are fewer than those in the Jehol and Yanliao biotas, many plant,

Central Asian orogenic belt (CAOB) records the collision his- invertebrate, and vertebrate footprint fossils, as well as a few

tory of the NCC with the Siberian Craton (Xiao et al., 2003). The vertebrate fossils, have been found in the lower-middle part of

Mongolia–Okhotsk orogenic belt (MOOB), located between the red beds (Figs. 3 and 4). Well-preserved coniferous petriﬁed

H. Xu et al. / Palaeoworld 26 (2017) 403–422 405

Fig. 1. (A) Skeleton map shows the distribution of the tectonic units mentioned in the paper (modiﬁed after Jahn et al., 2000 and Zheng et al., 2013). CAOB: Central

Asian orogenic belt; NCC: North China Craton; SC: Siberia Craton; SCC: South China Craton; YYOB: Yinshan–Yanshan orogenic belt. (B) Geological map of

northern North China and southern Central Asian orogenic belt. (C) Distribution of the Jurassic–Cretaceous transition red beds in the northern North China Craton

(modiﬁed after H. Xu et al., 2011).

woods represented by Xenoxylon latiporosum are present in the 3. Sedimentary facies

lower part of the Houcheng Formation in western Beijing (Duan,

1986). Invertebrate, consisting of conchostracans and ostracods, We measured 15 stratigraphic sections within the Tuchengzi/

and insect fossils have been reported in the lower-middle part Houcheng/Daqingshan Formation, including sections 1–6 in the

of the Tuchengzi/Houcheng Formation in western Liaoning– Chaoyang-Beipiao Basin in eastern YYOB, sections 7–12 in

northern Hebei. Wang and Li (2008) divided the conchos- the Shangyi Basin in central YYOB, and sections 13–15 in the

tracans into the Pseudograpta–Sinograpta–Monilesthera and Shiguaizi Basin in western YYOB. Sedimentary facies was ana-

the Yanshanoleptestheria–Pingquania–Linagyuanella assem- lyzed from these measured sections, which form ﬁve facies units,

blages. W.L. Wang et al. (2004) erected the Cetacella substriata– i.e., the alluvial, ﬂuvial, deltaic, lacustrine, and eolian units.

Mantelliana alta–Darwinula bapanxiaensis and the Djungarica

yangshulingensis–Mantelliana reniformis–Stenestroemia yang-

shulingensis assemblages for the ostracods. Sparse dinosaur 3.1. Alluvial unit

bones represented by Chaoyangsaurus youngi and Xuan-

huasaurs niei were discovered in the lower-middle part of the 3.1.1. Description

red beds (X.J. Zhao et al., 2006) (Figs. 3 and 4). Some unre- The alluvial unit is widely distributed in the lower and middle

ported sauropod dinosaur bones were found in the lower part of parts of the red beds. It consists of massive or thick-bedded con-

the Houcheng Formation in Xinghe, Inner Mongolia in recent glomerates, which are poorly sorted, normally graded, and clast-

years (Y.Q. Liu et al., 2012b). In contrast to the small amount of or matrix-supported (Fig. 5). The matrix is composed of poorly

dinosaur bone fossils, abundant footprints of small-sized thero- sorted mud, silt, and sand. The gravels ranging from granules to

pod dinosaurs, sauropod dinosaurs, and birds have been found boulders are angular–subangular in shape, and the largest boul-

in the lower-middle part of the Tuchengzi/Houcheng Formation ders are as large as 2.2 m in diameter (Fig. 5D). Crudely bedded

in northern Hebei–western Liaoning (Y.Z. Zhang et al., 2004; or lenticular coarse-grained sandstones are interbedded in the

Lockley et al., 2006; X.J. Zhao et al., 2006; Fujita et al., 2007; conglomerate (Fig. 5A). Lenticular conglomerate with cross-

Sullivan et al., 2009; Xing et al., 2009, 2011, 2012, 2014; Y.Q. bedding and erosive base, cross-bedded sandstone, thin-bedded

Liu et al., 2012b; J.P. Zhang et al., 2012) (Figs. 3 and 4). siltstone, and imbricated pebbles also occur in the conglomerate.

406 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 2. Representative Jurassic–Early Cretaceous stratigraphic successions and regional correlation in the northern North China Craton (modiﬁed after H. Xu et al.,

2013b).

3.1.2. Interpretation massive siltstone and mudstone with marl and limestone inter-

This unit is interpreted as alluvial fan deposits. The massive, layers. The conglomerate is normally graded, clast supported,

disorganized, poorly sorted, and subangular–angular conglom- and sandy ﬁlled with erosive base cutting into underlying beds.

erate is consistent with debris ﬂow as well as relatively rapid The pebbles are poorly sorted, and subangular in shape (Fig. 6A).

sedimentation and high energy ﬂow (Nemec and Steel, 1984; Small-scale cross-stratiﬁed sandstone lenses or planar-bedded

Postma, 1984). The crude bedded or sheet-like coarse-grained sandstones overlying imbricated gravels are interbedded with

sandstone with normal grading is interpreted as sheet ﬂood conglomerate (Fig. 6B). Some ﬁner-grained conglomerates

deposits under waning ﬂow conditions (Blair and McPherson, rested on lenticular conglomerates are trough or planar cross-

1994). Lenticular conglomerates with scoured bases, imbricated stratiﬁed and are overlain by planar cross-bedded sandstone

pebbles, and planar cross-bedded sandstones interbedded within (Fig. 6C). The bedded sandstone is normally graded and some-

conglomerates represent the channel ﬁll cutting into the root fan times alternates with planar cross-bedded sandstone or overlies

(Blair, 1999). Coarse sandstone lenses or wedge-shaped sand on bedded conglomerate. Channelized sandstones are planar or

units interbedded in the conglomerate might have been caused trough cross-bedded with scoured bases and gravel lags. They

by low water accretion in the braided channel (Miall, 1977). rest on the ﬁne-grained sandstone and siltstone or they are

interbedded within thick-bedded siltstone and claystone (Fig. 6D

and E). Caliche nodules, marls, and wormtrails are common in

3.2. Fluvial unit

the siltstone and mudstone (Fig. 6F and G).

3.2.1. Description

The ﬂuvial unit, composed of braided river, meandering river, 3.2.2. Interpretation

and ﬂood plain deposits, is widespread in the red beds. It con- The lenticular pebble–granule conglomerates with scoured

sists of channelized or lenticular conglomerate, cross-bedded bases are interpreted as channel lag deposits resulting from bed

conglomerate, sandstone, siltstone, and well-laminated or load (Allen, 1965; Hein and Walker, 1977). The channelized

H. Xu et al. / Palaeoworld 26 (2017) 403–422 407

Fig. 3. Integrated stratigraphic succession and characteristic fossils of the Jurassic–Cretaceous transition red beds in northern Hebei–western Liaoning.

Fig. 4. Representative lithology of the Tuchengzi/Houcheng/Daqingshan Formation in the northern North China (modiﬁed after H. Xu et al., 2014). K1b: Early

Cretaceous Bainüyangpan Formation; K1d: Early Cretaceous Dabeigou Formation; K1y: Early Cretaceous Yixian Formation; K1z: Early Cretaceous Zhangjiakou

Formation; J3-K1d: Late Jurassic–Early Cretaceous Daqingshan Formation; J3-K1h: Late Jurassic–Early Cretaceous Houcheng Formation; J3-K1t: Late Jurassic–Early

Cretaceous Tuchengzi Formation; J2-3t: Middle Jurassic–Late Jurassic Tiaojishan Formation; P2e: Middle Permian E’litu Formation; O1y: Early Ordovician Yeli

Formation; Jxw: Mesoproterozoic Wumishan Formation; Ar3-Pt1h: Neoarchean–Paleoproterozoic Huai’an Complex; Ar3w: Neoarchean Wulashan Group.

408 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 5. Photos show features of the interpreted alluvial fan deposits. (A and B) Massive or crudely bedded pebble-cobble conglomerate interbedded with lenticular

coarse-grained sandstone in the middle part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (C) Massive pebble-cobble conglomerate in the middle part

of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (D) Massive–thick-bedded boulder–cobble conglomerate in the lower part of the Houchengzi Formation

in the Shangyi Basin; the largest gravel exceeds 2.2 m in diameter. (E–G) Massive–thick-bedded cobble conglomerate in the lower part of the Daqingshan Formation

in the Shiguaizi Basin.

conglomerates with scoured bases and trough cross-bedded braided river (Miall, 1977). In contrast, the association of chan-

conglomerates represent channel ﬁll. The crudely bedded con- nel lag deposits, point bar deposits, and thick ﬂood plain or

glomerate with imbrication and normal grading is indicative of overbank deposits are interpreted as meandering river deposits

longitudinal bars (R.D. Smith, 1970; Rust, 1972; Miall, 1985). (Walker and Cant, 1984).

Planar-bedded coarse-grained sandstone overlying the conglom-

erate was probably generated by the waning ﬂow during ﬂood 3.3. Deltaic unit

stage on the surfaces of longitudinal bars. Trough cross-bedded

sandstone is considered the product of channel ﬁll or sinuous- 3.3.1. Description

crested dunes (Walker and Cant, 1984). Planar cross-bedded The deltaic unit is present in the lower and upper parts

sandstone is consistent with linguoid or transverse bars, repre- of the Tuchengzi Formation and contains two different litho-

senting avalanche-slope progradation (Miall, 1977; Walker and logical successions. The ﬁrst is characterized by massive or

Cant, 1984). When the cross-beds have large scoured surfaces thick-bedded conglomerates interbedded in the thick-bedded

and are overlain by thick mudstone or siltstone, they can be inter- mudstone and siltstone (Fig. 7A). The conglomerate is nor-

preted as point bars (Collinson, 1970; Smith, 1974; Levey, 1977). mally graded, clast-supported with scoured base, and is

The thick bedded siltstone and mudstone with abundant worm- present at the upper part of the lithological succession. The

trails, caliche nodules, and marl interlayers are linked to ﬂood gravels ranging from granules–cobbles are poorly sorted,

plain or overbank deposits. The small-scale channelized sand- angular–subangular in shape (Fig. 7A). Medium–thick bed-

stone interbedded in the thick-bedded siltstone and mudstone ded coarse-grained sandstone with planar cross-bedding rests

is consistent with crevasse splay (Fielding, 1986; Smith et al., on the conglomerate and is overlain by thick-bedded siltstone

1989). The sequences of channel lag deposits or scoured ﬁlled and mudstone. Some lenticular conglomerate and sandstone

deposits at the base, capped by thick longitudinal bar deposits with scoured base and cross-beddings are interbedded in the

and thin ﬂood plain deposits, are consistent with braided river medium–thick bedded ﬁne-grained sandstone and siltstone. The

deposits (Cant and Walker, 1976; Miall, 1977). The assembly second unit, in an ascending order, consists of structureless mud-

of linguoid and transverse bar sandstone is typical of a sandy stone, laminated ﬁne-grained sandstone, planar cross-bedded

H. Xu et al. / Palaeoworld 26 (2017) 403–422 409

Fig. 6. Photos show features of the interpreted ﬂuvial deposits. (A) Lenticular cobble conglomerate with erosive bases overlain by planar bedded or small lenses of

coarse-grained sandstone in the lower part of the Daqingshan Formation in the Shiguaizi Basin. (B) Trough cross-bedded conglomerate with poorly sorted, angular

pebble–cobbles and scour base in the upper part of the Daqingshan Formation in the Shiguaizi Basin. (C) Sandy conglomerate with planar cross-bedding overlying

on planar bedded pebble conglomerate in the lower part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (D) Thick-bedded coarse-grained sandstone

with trough cross-bedding of the Daqingshan Formation in the Shiguaizi Basin. (E) Thick-bedded coarse-grained sandstone with planar cross-bedding overlying on

the lenticular conglomerate with scour base of the Houcheng Formation in the Shangyi Basin. (F) Thick-bedded mudstone with abundant calcareous nodules and

marls in the middle part of the Daqingshan Formation in the Shiguaizi Basin. (G) Thick-bedded siltstone with abundant calcareous nodules in the middle part the

Houcheng Formation in the Shangyi Basin. (H) Thick-bedded mudstone and siltstone in the lower-middle part of the Tuchengzi Formation in the Chaoyang-Beipiao

Basin. (A), (D), and (F) are cited from H. Xu et al. (2011, 2013b).

ﬁne-grained sandstone, trough cross-bedded medium-grained and Wescott, 1984; Soegaard, 1990; McCallum and Robertson,

sandstone, a limestone interlayer, and coarse–medium-grained 1995). The disorganized conglomerate present at the upper

sandstone with planar cross-bedding and muddy intraclasts. part of the sequence resting on the siltstone is interpreted as

The medium–thick-bedded medium–coarse-grained sandstone debris ﬂow in the delta plain. The massive and thick-bedded

is channelized with trough and planar cross-beddings. It rests granule conglomerates with scoured bases interbedded in the

on the siltstone with erosive base (Fig. 7B and C). The planar thick-bedded siltstone and mudstone are attributed to subaque-

coarse-grained sandstone with a scoured base, muddy intra- ous debris ﬂow (Flores, 1975; Galloway, 1976; Wescott and

clasts, and planar cross-bedded sandstone constitute a ﬁning Ethridge, 1980; Ethridge and Wescott, 1984). The planar-bedded

upward sequence (Fig. 7D). Soft deformation and ripple cross- coarse-grained sandstone overlying the conglomerate with nor-

bedding are present in the thick-bedded ﬁne-grained sandstone, mal grading resulted from a waning, sediment-laden stream

which grades into alternation of medium–thin-bedded ﬁne- ﬂow (Mutti et al., 1996). The thick-bedded mudstone repre-

grained sandstone and mudstone (Fig. 7E–I). sents suspension settling in the prodelta. The sandy braided delta

consists of braided channel ﬁlling, longitudinal bar deposits

3.3.2. Interpretation in the delta plain, subaqueous distributary channel and inter-

The two lithological successions have been distinguished as channel mudstone, sand sheet deposits in the delta front, and

a fan delta and a sandy braided delta. The fan delta is character- mudstone in the prodelta. The muddy intraclasts and massive

ized by debris ﬂow in the fan delta plain, subaqueous debris sandstones with scoured bases represent the channel ﬁlls. The

ﬂow in the delta front, and thick-bedded siltstone and mud- planar cross-bedded sandstone is related to longitudinal bars

stone in the prodelta (Wescott and Ethridge, 1980; Ethridge resulting from frontal aggression (Miall, 1977). The channel

410 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 7. Photos show features of the interpreted deltaic deposits. (A) Lenticular cobble conglomerate and planar coarse-grained sandstone interbedded in the ﬁne-grained

sandstone and siltstone in the lower part of the Houcheng Formation in the Shangyi Basin. (B) Thick-bedded medium-grained sandstone with planar cross-bedding

in the lower part of the Houcheng Formation in the Shangyi Basin. (C) Lenticular planar cross-bedded ﬁne–medium-grained sandstone overlain by thick-bedded

coarse–medium-grained sandstone with trough and planar cross-beddings in the lower part of the Houcheng Formation in the Shangyi Basin. (D) Alternation of

lenticular medium–ﬁne-grained sandstone with planar cross-bedding and medium–thick-bedded mudstone in the upper part of the Tuchengzi Formation in the

Chaoyang-Beipiao Basin. (E) Thick-bedded ﬁne-grained sandstone with soft-sediment deformation overlain by alternation of medium–thin-bedded ﬁne-grained

sandstone and mudstone in the upper part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (F) Lenticular or medium-bedded medium–ﬁne-grained

sandstone interbedded with thin-bedded mudstone overlain by alternation of thin-bedded ﬁne-grained sandstone and mudstone in the upper part of the Tuchengzi

Formation in the Chaoyang-Beipiao Basin. (G) Fine-grained sandstone with soft-sediment deformation overlain by wave cross-bedded ﬁne-grained sandstone in the

lower part of the Houcheng Formation in the Shangyi Basin. (H) Fine-grained sandstone with wave cross-bedding in the lower part of the Houcheng Formation in

the Shangyi Basin. (I) Fine-grained sandstone with soft-sediment deformation in the lower part of the Houcheng Formation in the Shangyi Basin.

ﬁll and longitudinal bars comprise a sandy braided river in medium–thick-bedded ﬁne-gained sandstone is normally graded

the delta plain. Channelized medium-grained sandstone with with wave and planar cross-bedding. The clasts are well sorted

trough cross-bedding overlain by limestone probably occurred and subangular in shape. The sandstone laterally persists up

in the delta front as interdistributary channel deposits. The thick- to tens of meters (Fig. 8A–C). Symmetric ripple marks with

bedded ﬁne-grained sandstone with soft-sediment deformation straight or sinuous ridges, round troughs, and sharp crests occur

and ripple cross-bedding is interpreted as a mouth bar. The bed- on the ﬁne-grained sandstone, which is intercalated in the thick-

ded siltstone and ﬁne-grained sandstone may be attributed to bedded mudstone (Fig. 8D and E).

a frontal sand sheet. The thick-bedded mudstone is considered

the product of suspension settling in the prodelta (Elliott, 1974;

3.4.2. Interpretation

Fielding, 1984).

The cross-bedded ﬁne-grained sandstone is considered to

have been formed by wave ﬂow along the shore (Clifton et al.,

3.4. Lacustrine unit 1971; Hadlari et al., 2006). The laminated ﬁne-grained sand-

stone may be the product of the upper ﬂow regime (Kraus and

3.4.1. Description Gwinn, 1997). The symmetric ripple marks are consistent with

The lacustrine unit is characterized by laminated mud- wave ripples formed in the nearshore setting. The laminated

stone, marls, siltstone, and ﬁne-grained sandstone. The mudstone and marls are interpreted as offshore deposits due to

H. Xu et al. / Palaeoworld 26 (2017) 403–422 411

Fig. 8. Photos show features of the lacustrine deposits. (A) Thin–medium-bedded ﬁne-grained sandstone with wave cross-bedding interbedded with thin-bedded

mudstone with mud cracks in the upper part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (B) Medium-bedded ﬁne-grained sandstone with small-

scale wave cross-bedding in the upper part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (C) Yellow–green thin/medium-bedded medium/ﬁne-grained

sandstone with trough and planar cross-beddings interbedded in siltstone in the lower part of the Houcheng Formation in the Shangyi Basin. (D) Thick-bedded

mudstone interbedded with medium-bedded ﬁne-grained sandstone with planar cross-bedding in the upper part of the Tuchengzi Formation in the Chaoyang-Beipiao

Basin. (E) Medium-grained sandstone with ripple marks in the lower part of the Tuchengzi Formation in the Chaoyang-Beipiao Basin. (F) Fine-grained sandstone

with ripple marks in the upper part of the Houcheng Formation in the Shangyi Basin. (B) and (E) are cited from H. Xu et al. (2011).

settling of suspended sediments from water bodies (Wünderlich, attributed to eolian sinuous-crested dunes and linguoid or trans-

1972; Vanden Berg, 1977; Scherer et al., 2007). verse dunes, respectively (McKee, 1980; Rubin, 1987). The

low-angle cross-bedded sandstone with normal grading is con-

sistent with eolian sand sheets generated by grainfall on the

3.5. Eolian unit

interdune (Scherer and Lavina, 2005; Mountney, 2006). The rip-

ple marks with coarser-grained crests and ﬁner-grained troughs

3.5.1. Description

represent wind ripples. The inversely graded medium-grained

This unit commonly occurs in the upper part of the Tuchengzi

sandstone interbedded in the foresets is interpreted as grain-

Formation in western Liaoning. In fact, the eolian deposits are

ﬂow resulting from dune advances through repeated avalanching

also present in the upper part of the Houcheng Formation in the

of an active slipface (Hunter, 1977; Kocurek and Dott, 1981;

Shangyi Basin in northwestern Hebei, and the Santai Formation

Kocurek, 1991). The channelized sandy conglomerate cutting

in western Shandong (H. Xu et al., 2013a). The unit consists of

into cross-bedded sandstone is considered to have been formed

ﬁne- to medium-grained sandstone with sub-rounded grains, and

by an ephemeral braided river (Mountney et al., 1998).

is characterized by large-scale planar and trough cross-beddings

organized into 0.5–3-m-thick sets (Fig. 9A–C). Ripple marks

with coarser-grained crests and ﬁner-grained troughs occur on 4. Provenance

the cross-bedded sandstone (Fig. 9D). Internally, the bounding

surfaces of the cross-bedded units are planar, and the foreset lam- Paleocurrent indicators were measured from cross-beddings

◦

inae are curved with dip angles ranging of 10–30 (Fig. 9A–C). and imbricated pebbles in the outcrops. The rose diagram shows

Inversely graded medium-grained sandstones are intercalated in the direction of paleocurrent orientation. Detrital composition

the foresets. In contrast, normal-graded ﬁne-grained sandstones is based on the analysis of conglomerate clasts. At each site

characterize the low-angle cross-beddings with foreset dip investigated, at least 150–100 pebble counts were identiﬁed in

◦ 2

angles up to 10 (Fig. 9E). Lenticular sandy conglomerates with 1 m and plotted on a pie diagram.

subangular–angular, poorly sorted, and clast-supported gravels

are present in the trough cross-bedded sandstone (Fig. 9F).

4.1. Chaoyang-Beipiao Basin

3.5.2. Interpretation The Chaoyang-Beipiao Basin is located in the eastern YYOB

The presence of well-sorted, ﬁne–medium-grained sandstone (Fig. 1C). Basement of the basin is composed mainly of

with large-scale cross-beddings is interpreted as eolian deposits. Mesoproterozoic–Early Neoproterozoic dolomite and siliceous

The large-scale trough and planar cross-bedded sandstones are rock, Early Paleozoic limestone and siliceous rock, and

412 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 9. Photos show features of the interpreted eolian deposits. (A) Large scale trough cross-bedded ﬁne-grained sandstone in the upper part of the Tuchengzi Formation

in the Chaoyang-Beipiao Basin. (B) Large-scale planar and trough cross-bedded medium-grained sandstone with scoured-like bounding surfaces truncating cosets

in the upper part of the Houcheng Formation in the Shangyi Basin. (C) Large-scale planar cross-bedded medium-grained sandstone with high dips. (D) Ripple

marks with coarser grained crest and ﬁner grained trough present on the surface of cross-bedded sandstone in the upper part of the Tuchengzi Formation in the

Chaoyang-Beipiao Basin. (E) Normal graded ﬁne-grained sandstones with low angle cross-beddings in the upper part of the Houcheng Formation in the Shangyi

Basin. (F) Sandy ﬁlled lenticular conglomerate interbedded in the trough cross-bedded medium-grained sandstone in the upper part of the Tuchengzi Formation in

the Chaoyang-Beipiao Basin. (A), (D), and (F) are cited from H. Xu et al. (2011, 2013a).

Late Paleozoic–Middle Triassic clastic rock. It is ﬁlled with 4.2. Shangyi Basin

Late Triassic–Cretaceous volcanic-sedimentary cyclic sedi-

ments (Fig. 2). The Tuchengzi Formation, as the most widely The Shangyi Basin, located at the middle part of the

exposed strata in the basin, overlies unconformably the basement YYOB (Fig. 1C), is ﬁlled mainly with the Early–early Mid-

rocks or conformably the Tiaojishan/Lanqi Formation. The latter dle Jurassic and Late Jurassic–Early Cretaceous deposits.

consists predominantly of andesitic rocks. The basement of the Shangyi Basin consists mainly of

Conglomerate of the Tuchengzi Formation consists mainly Neoarchean–Paleoproterozoic metamorphic rocks, including

of clasts of andesitic volcanic rocks with subordinate amounts the Khondalite to the west, the metamorphic volcanic-

of clastic rocks, siliceous rocks, carbonate, tuff, and granite sedimentary rocks of the Hongqiyingzi Group emplaced by

(Fig. 10). The andesitic clasts (18–77.1%) are dominant in the Paleoproterozoic and Late Paleozoic granitic rocks to the north,

basal part of the Tuchengzi Formation and gradually decrease and the gray gneiss of the Huai’an Complex to the south. More-

in abundance upward. The clasts are comparable to the andesite over, the Mesoproterozoic carbonate and clastic rocks are also

of the underlying Tiaojishan Formation. The carbonate clasts present in the north of the basin. The Houcheng Formation

appear from the middle part of the Tuchengzi Formation and is widely distributed in the basin, which is disconformably

dominate (70%) in section 2 (Figs. 1C and 10), indicating ero- or unconformably overlies the metamorphic basement or the

sion of the Mesoproterozoic Changcheng and Jixian Systems Early–early Middle Jurassic deposits.

since the deposition of the middle part of the Tuchengzi For- Conglomerates are widely distributed in the Houcheng For-

mation. Section 6 markedly shows changes in the conglomerate mation at the northern, western, and southern margins of

composition of the Tuchengzi Formation. From the lower part to the basin. The clasts of the conglomerates vary in differ-

the middle part of the Tuchengzi Formation, the andesitic clasts ent locations. In section 7, clasts are composed of granite

decrease from 77.1% to 33.3%, while the clastic rocks and car- (41–50%), granitic gneiss (15–39%), gneiss (4–29%), and small

bonate clasts increase from 10.5% and 1.1% to 42% and 14%, amounts of greywacke and quartzite (Fig. 11). The clasts could

respectively (Fig. 10). These changes suggest unroofed erosion correlate with the Paleoproterozoic–Late Paleozoic granitic

that took place from the young strata to the old strata. Moreover, rocks, the Hongqiyingzi Group, and the Mesoproterozoic clas-

the clastic and siliceous clasts are considered to have derived tic rocks of the basement, respectively. In section 8, clasts

from the Mesoproterozoic–Early Paleozoic strata, and the small of the boulder–cobble conglomerate comprise granitic gneiss

amount of granite (3.1–4%), only present in sections 2 and 6, (14–42%), gneiss (39–78%), and schist (5–11%) (Fig. 11). The

may be attributed to the Permian–Triassic granites outcropping proportion of granitic gneiss clasts markedly decreases in con-

in the northwest of the basin. These inferences are consistent trast to the increase of the proportion of the clasts of gneisses

with paleocurrent orientations (Fig. 10). upward through the section, indicating unroofed erosion of the

H. Xu et al. / Palaeoworld 26 (2017) 403–422 413

Fig. 10. Measured stratigraphic sections of the Tuchengzi Formation in the Chaoyang-Beipiao Basin show the depositional sequence, paleocurrent orientation, clast

composition of conglomerate and interpreted sedimentary facies. m: mud; s: silt; fs: ﬁne sand; ms: medium sand; cs: coarse sand; g: granules; p: pebbles; c: cobbles.

metamorphic rocks of the Hongqiyingzi Group and the intruded 4.3. Shiguaizi Basin

granitic rocks. These two inferences are consistent with south-

eastward and southwestward paleocurrents. In section 9, the The Shiguaizi Basin is located in the western YYOB

clasts consist mainly of gneiss (40%) and granitic gneiss (46%) (Fig. 1C). The Neoarchean granulite and gneiss, Paleopro-

with subordinate amounts of quartzite (6%), greywacke (5%), terozoic khondalite, and Paleoproterozoic–Early Mesozoic

and granite (3%) (Fig. 11). The paleocurrents are southeastward granitoid rocks are well exposed around the basin, especially

oriented. The clast types and paleocurrent orientation imply in the northern area. In contrast, the Mesoproterozoic dolomite

that the sediment sources may have derived from the Paleo- and clastic rocks and Early Paleozoic limestone are distributed

proterozoic granitic rocks and the Hongqiyingzi Group in the in the south of the basin. The Shiguaizi Basin is ﬁlled with the

north and the Khondalite rock series in the west. In section Early Triassic and Early Jurassic–Early Cretaceous volcanic-

11, clasts are composed mainly of gneiss (47.8%), granulite sedimentary rocks dominated by clastic rocks. The Early and

(14.5%), greywacke (10.1%), granite (9.4%), and granitic gneiss Middle Jurassic coal-bearing rocks are prograded from west to

(5.8%) (Fig. 11). Combined with westward and northwestward east; in contrast, the Late Jurassic–Early Cretaceous Daqingshan

paleocurrent orientations, the clasts may be correlated with the Formation developed from north to south.

Huai’an complex exposed in the south of the basin. In section Conglomerates of the Daqingshan Formation consist mainly

12, clasts consist predominantly of granite (66%) and granulite of metamorphic rocks, siliceous rocks, sandstone, and lime-

(23%) with small amounts of quartzite, schist, volcanic rocks, stone. The metamorphic clasts represented by gneiss, quartzite,

gneiss, and sandstone clasts (Fig. 11). In combination with east-, and greywacke rocks gradually increase in abundance upward

southeast-, and north-directed paleocurrents, this indicates that and reach 98% in the upper part of the Daqingshan Formation

the granites exposed to the northwest of the basin and granulite, (Figs. 5F and 12). In combination with the south-directed pale-

quartzite, schist, and gneiss present to the south of the basin were ocurrents, the Neoarchean and Paleoproterozoic metamorphic

likely the dominant sources. rocks mainly present to the north of the basin should be the

414 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 11. The measured stratigraphic sections of the Houcheng Formation in the Shangyi Basin, showing the depositional sequence, paleocurrent orientation,

conglomerate composition and interpreted sedimentary facies. m: mud; s: silt; fs: ﬁne sand; ms: medium sand; cs: coarse sand; g: granules; p: pebbles; c: cobbles.

Fig. 12. The measured stratigraphic sections of the Daqingshan Formation in the Shiguaizi Basin, showing conglomerate composition and interpreted sedimentary

facies. m: mud; s: silt; fs: ﬁne sand; ms: medium sand; cs: coarse sand; g: granules; p: pebbles; c: cobbles.

H. Xu et al. / Palaeoworld 26 (2017) 403–422 415

Fig. 13. Paleocurrent orientations and lithofacies of the Jurassic–Cretaceous transition red beds in northern North China (green and purple paleocurrent orientations

of the Houcheng Formation in Lingyuan, Chengde, Shouwangfen, Xinchengzi, Luanping, and Chicheng are derived from Cope, 2003; S.F. Liu et al., 2004; Qu et al.,

2006; Z. Li et al., 2007; black paleocurrent orientations are based on this paper). (For interpretation of the references to color in this ﬁgure legend, the reader is

referred to the web version of this article.)

dominant source for these metamorphic clasts. In contrast, the and Mesoproterozoic–Early Paleozoic carbonate, siliceous, and

proportion of siliceous, sandstone and limestone clasts gradu- clastic rocks. These inferences are supported by the conver-

ally decrease upward. Siliceous and sandstone clasts only occur gent paleocurrents of the Houcheng Formation in the Chengde

in the lower part of the Daqingshan Formation and account for Basin (Fig. 13). Moreover, the changes in the conglomerate

approximately 28%. The proportion of limestone clasts (4–11%) composition of the Houchengzi Formation indicate erosional

increases upward to the middle part, and then decreases to sequences from the Middle–Late Jurassic Tiaojishan Formation

2% in the upper part (Fig. 11). These features indicate that to Early Paleozoic–Mesoproterozoic sedimentary rocks to Pale-

the Mesoproterozoic and Early Paleozoic sedimentary rocks oproterozoic metamorphic rocks. In the Shouwangfen Basin,

distributed to the south of the basin is a subordinate source the conglomerate clasts of the Houcheng Formation consist pre-

for these sedimentary rocks for the Daqingshan Formation. dominantly of volcanic rocks, with small amounts of granite

Thus, clasts of the Daqingshan Formation were derived from and granitic gneiss in the lower part and carbonate, siliceous,

Neoarchean–Paleoproterozoic metamorphic rocks and Meso- volcanic, and clastic rocks in the upper part (S.F. Liu et al.,

proterozoic and Early Paleozoic sedimentary rocks present to 2004, 2007). Combined with the south-directed paleocurrents

the north and south of the basin respectively in the early stage, (Fig. 13), this suggests that the sources of the Houcheng For-

and then it was dominated by the metamorphic rocks distributed mation were derived mainly from the Tiaojishan Formation and

to the north of the basin. Mesoproterozoic–Early Paleozoic strata present in the north of

the basin.

4.4. Other basins in the YYOB

5. Discussion

Previous researchers have conducted many studies on

the provenances of the Houcheng Formation in the central 5.1. Paleogeography

YYOB, such as in the Chengde Basin, Luanping Basin, and

Shouwangfen Basin. In the Chengde Basin, the sources of the In early Mesozoic, a uniﬁed Ordos–North China basin was

Houcheng Formation appear to be quite different from the north formed in northeast Asia (Y.T. Yang et al., 2005; Y.Q. Liu et al.,

to the south. In the north of the basin, the conglomerate clasts 2015). The subsequently uplifted CAOB acted as one of the

consist mainly of volcanic, granitic, metamorphic, and clastic main sediment provenances for the uniﬁed Ordos–North China

rocks, with an absence of carbonate and siliceous rocks (S.F. basin (J.H. Yang et al., 2006; S.W. Xie et al., 2012; Li and Huang,

Liu et al., 2004, 2007; Qu and Zhang, 2005; Qu et al., 2006; 2013; Li et al., 2013; S.F. Liu et al., 2013). The late Middle Juras-

He et al., 2007; J. Liu et al., 2013, 2014). This feature indicates sic intracontinental orogeny (Yanshan movement) in the NCC,

that the clasts are in good agreement with the volcanic rocks characterized by intense thrusting and magmatism, resulted in

of the Tiaojishan Formation and Neoarchean–Paleoproterozoic the formation of the east–west-trending YYOB (Davis et al.,

metamorphic rocks and magmatic rocks widely exposed in the 1998, 2001; J. Liu et al., 2012). Since then, the previously

north of the basin. In contrast, in the south of the basin, the uniﬁed Ordos–North China basin diverged, and the differen-

conglomerate clasts are composed predominantly of volcanic tial evolution of basins and paleogeography between eastern

rocks and carbonate, with subordinate amounts of clastic and and western North China was initiated (Y.Q. Liu et al., 2015).

siliceous rocks (S.F. Liu et al., 2004, 2007; Qu and Zhang, Based on detrital zircon provenance analysis on the deposits

2005; Qu et al., 2006; He et al., 2007; J. Liu et al., 2013, 2014), in Western Hills in Beijing, J.H. Yang et al. (2006) proposed

consistent with the volcanic rocks of the Tiaojishan Formation that the sediment provenance of the Jingxi Basin in the northern

416 H. Xu et al. / Palaeoworld 26 (2017) 403–422

Fig. 14. Cartoon shows the paleogeographic reconstruction, sediment provenance and tectonic setting of the Jurassic–Cretaceous transition red beds in the northern

North China Craton. YYOB: Yinshan–Yanshan orogenic belt.

NCC gradually shifted from the CAOB to the northern edge of in the northern NCC (Figs. 13 and 14). In addition, the occur-

the NCC after the sedimentation of the lower Middle Jurassic rence of a series of Late Jurassic–Early Cretaceous rift basins

Shangyaopo/Longmen Formation. This is a direct response to in Mongolia may be indicative of a large-scale collapse of the

the uplift of the YYOB. CAOB. Therefore, the east–west-trending YYOB may be the

Sedimentary facies analyses indicate that the J-K tran- main paleogeographic highland at the northern margin of the

sition red beds in northern North China consist mainly of NCC during Late Jurassic–Early Cretaceous (Fig. 14).

alluvial and ﬂuvial deposits, suggesting local high-gradient

depositional systems (S.F. Liu et al., 2007). Results of the 5.2. Paleoenvironment

provenance analysis show that the sediments of the red beds

were derived mainly from the bed rocks of the basins, espe- The new discoveries from the Yanliao and Jehol biotas in

cially in the north. In western Liaoning–northern Hebei, the Northeast China during the past 20 years have increased our

conglomerates of the Tuchengzi/Houcheng Formation are com- knowledge about the evolution of terrestrial organisms in Meso-

posed predominantly of volcanic rocks, indicative of origin zoic, such as the origin of birds, the evolution of feathers and

from the underlying Tiaojishan Formation that is widely dis- ﬂight, and the early evolution and diversiﬁcation of mammals,

tributed in northern Hebei–western Liaoning. This suggests dinosaurs, and angiosperms (Zhou et al., 2003; Zhou, 2006). Ear-

the sources are proximal. The Mesoproterozoic–Early Paleo- lier studies referred to the Yanliao Biota as a “Pre-Jehol Biota”

zoic carbonate, siliceous, and clastic clasts start appearing from (J.F. Zhang, 2002) and maintained that before the emergence of

the middle part of the Tuchengzi/Houcheng Formation and the Jehol Biota, over 90% of the biological genera and species

increase in abundance in the strata upward in the basins in the of the Yanliao Biota had disappeared from the Tuchengzi For-

central-eastern YYOB. This suggests that the basement of basins mation (Ji et al., 2004, 2006). About 9-Ma gap exists between

underwent an obvious uplift during Late Jurassic–Early Creta- the Yanliao Biota and the Jehol Biota, which is consistent with

ceous. Moreover, studies of detrital zircon geochronology of the the time span of the Tuchengzi Formation/Houcheng Formation

Tuchengzi/Houcheng/Daqingshan Formation in northern North in western Liaoning and northern Hebei (ca. 154–137 Ma, H.

China indicated that the detrital zircons were derived predomi- Xu et al., 2012). Therefore, the paleoenvironment and paleoe-

nantly from the magmatic and metamorphic rocks in the northern cology during the period of deposition of the transitional red

NCC rather than those in the CAOB (H. Xu et al., 2013b). These beds may contain key information concerning the relationship

features indicate that the YYOB, formed in late Middle Jurassic, and evolution of the Yanliao and the Jehol biotas.

experienced successive uplift in Late Jurassic–Early Cretaceous The paleoecology of the Yanliao Biota reconstructed by

and served as a barrier that prevented sources of the CAOB being insects suggests that abundant shallow-water lakes and swamps,

transported into the basins in the northern NCC. Paleocurrent along with adjacent mountains and mountain streams devel-

evidence in different localities shows characteristics of a local- oped in North China during the Middle Jurassic (P.J. Liu et al.,

ized convergent paleo-drainage system, suggesting that a series 2010). The plant fossils preserved in the Tiaojishan Forma-

of relatively independent small- to mid-scale basins developed tion consist mainly of fern, pine, and cycad (J.F. Zhang, 2002;

H. Xu et al. / Palaeoworld 26 (2017) 403–422 417

Jiang et al., 2012; Tian et al., 2014), suggesting a warm and evolved directly from Pseudograpta and Monilestheria in the

moist environment coexisted with seasonal aridity and semi- Tuchengzi/Houcheng Formation. The Yanliao Biota preserved

aridity in the Middle–Late Jurassic. The Tuchengzi Formation in the Jiulongshan and Tiaojishan formations also shares some

contains thick alluvial conglomerates, abundant calcareous nod- faunal components with the Jehol Biota (Zhou et al., 2010).

ules, mud cracks, gypsums, salt pseudomorphs, and paleosoils. These features imply that the Yanliao Biota has some special

The sporopollen ﬂora of the formation has high Classopollis relationships with the Jehol Biota. However, it is too early to

(>82.6%) but extremely low pine pollen and fern spores (<2–3%) assert that the Yanliao Biota is “Pre-Jehol Biota” or they are two

content. The latter two components are indicative of warm and evolutionary biotas. More fossils and works are needed to solve

humid climate (S.L. Zheng et al., 2001). These features reﬂect a this problem.

hot and dry climate in the J-K transition time. Large numbers of

dinosaur footprints and several bird footprints have been found 5.3. Tectonic evolution

in the Tuchengzi/Houcheng Formation in Chaoyang, Beipiao,

Chengde, Yanqing, Chicheng and Shangyi (Yabe et al., 1940; The basins containing the J-K transition red beds had been

Y.Z. Zhang et al., 2004; Chen et al., 2006; Lockley et al., considered to have been formed in an intensive regional com-

2006; Sullivan et al., 2009; Y.Q. Liu et al., 2012b; Xing et al., pressional tectonic setting (Davis et al., 1998, 2001; He et al.,

2012; J.P. Zhang et al., 2012). The dinosaur footprints con- 1998, 1999, 2007, 2008; S.F. Liu et al., 2004, 2007; Cope

sist dominantly of small-scale theropod footprints with a small et al., 2007; Z. Li et al., 2007; Dong et al., 2008; J. Liu et al.,

number of sauropod or ornithopod footprints, implying that the 2012, 2013, 2014). However, recent studies have shown that

severe environment signiﬁcantly inﬂuenced the plants and ver- the Tuchengzi/Houcheng Formation is an important constitu-

tebrates. Moreover, the top part of the Tuchengzi/Houcheng tional component of the giant rift system of Northeast Asia (ca.

Formation shows a regional eolian deposition controlled by 165/160–130 Ma) that overlies the YYOB (>ca. 165/160 Ma)

westward planetary wind systems that can be compared with (Y.Q. Liu et al., 2015; Qi et al., 2015). Geochronologic studies

desert deposition intercontinentally developed in mid-latitude indicated that the age of the Tuchengzi/Houcheng Forma-

regions in Late Jurassic–Early Cretaceous (H. Xu et al., 2013a). tion (154–137 Ma) overlaps that of the underlying Tiaojishan

Recently, we have also found typical Late Jurassic eolian sand- Formation (165–152 Ma) and the overlying Zhangjiakou For-

stone in Shanxi. The occurrence of regional eolian deposits may mation (143–130 Ma) (Fig. 3). This suggests that the Late

be consistent with the existence of a late Mesozoic East China Jurassic–Early Cretaceous volcanic-sedimentary basins were

Plateau proposed by previous workers based on different studies formed under similar tectonic setting. The Late Jurassic–Early

(Chen, 1979; Deng et al., 1996; Q. Zhang et al., 2001, 2008). Cretaceous volcanic rocks are not limited in the northern NCC

Recent studies on the J-K transition vesicular basalts in Inner but widely distributed in Northeast China (W.L. Xu et al.,

Mongolia indicated that the paleoaltimetry of the East China 2013). They gradually become younger and belong chemically

Plateau could reach 5000 m, as high as the present Tibet Plateau to calc–alkaline series and to a bimodal volcanic rock associ-

(Xia et al., 2012). In contrast, during the deposition period ation from north to south. They reﬂect an intracontinental rift

of the Zhangjiakou–Dabeigou–Yixian–Jiufotang formations, a environment (Fan et al., 2003; L.C. Zhang et al., 2008; Z.G.

temperate moist climate was inferred coexisted with mountains, Chen et al., 2009; Gou et al., 2010; E. Meng et al., 2011; W.L.

rivers, and lakes in Northeast China (Y.Q. Liu et al., 2009). Pale- Xu et al., 2013; S.Q. Li et al., 2014).

oclimatical analysis of the fossil wood assemblage indicated a Moreover, the Jurassic–Cretaceous magmatic rocks are also

cool and wet environment in western Liaoning during the Early widespread in North China and Northeast China. X.H. Zhang

Cretaceous (Ding et al., 2016). The presence of feathers in some et al. (2008) proposed that the peraluminous leucogranites

dinosaurs is a response to an adaptation to such a cool or cold (153 ± 5 Ma) emplaced in the Yiwulüshan MCC were formed

environment in the Early Cretaceous (X. Xu et al., 2012). in the intracontinental extension, suggesting regional exten-

The above-mentioned phenomena suggest that during the sion initiated after the Middle Jurassic orogeny. H.J. Xie et al.

transition period between the two biotas, the paleogeography (2012) proposed that the A-type granites (139.6 ± 1.7 Ma)

and paleoenvironment in northern China dramatically changed, were emplaced in Northeast China. Furthermore, a series of

characterized by the occurrence of eolian deposits. During this maﬁc dykes intruded into the Tuchengzi/Houcheng Forma-

period, due to the mountainy environment resulted from crust tion in northern Hebei–western Liaoning have been constrained

uplift and northwestward winds blowing year around, the cli- to 140–141 Ma by SHRIMP U-Pb dating (unpublished data

mate gradually changed to hot and arid in northern North China. from this study). The Jurassic–Cretaceous transition maﬁc

These changes caused catastrophic events for the Yanliao Biota, dykes (144 ± 2 Ma, 143 ± 2 Ma by SHRIMP U-Pb dating) also

which probably only a few species survived in a few inter- intruded into the Santai Formation in western Shandong (S. Liu

mountain basins. In the earliest Cretaceous, frequent volcanism et al., 2008), which is considered to be contemporary with the

must have created a series of small-scale pools and provided Tuchengzi/Houcheng Formation (H. Xu et al., 2013a). All these

abundant nutrients, which is beneﬁcial for the emergence of lines of evidence suggest an extensional tectonic setting related

the Jehol Biota (Wang, 1990). In fact, some fossils from the to the post-orogenic collapse of the MOOB (Ying et al., 2010;

Tuchengzi/Houcheng Formation have close relationships with W.L. Xu et al., 2013) (Fig. 14). This inference is consistent

those of the Jehol Biota. Wang et al. (2013) proposed that with the evolution of MCCs in the CAOB and NCC charac-

the Nestoria and Sentetheria in the Dabeigou Formation were terized by T. Wang et al. (2012) and others. The intensity of

418 H. Xu et al. / Palaeoworld 26 (2017) 403–422

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