Journal of Asian Earth Sciences 114 (2015) 611–622

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Journal of Asian Earth Sciences

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Late to Early sedimentary-tectonic development in the Basin, Yanshan fold-thrust belt, North Craton ⇑ Jian Liu a,b, , Yue Zhao a, Ankun Liu a, Hao Ye a a Institute of Geomechanics, Chinese Academy of Geological Sciences, Beijing 100081, China b Key Laboratory of Paleomagnetism, Chinese Academy of Geological Sciences, Beijing 100081, China article info abstract

Article history: The Chengde Basin is located in the central part of the Yanshan fold-thrust belt in the northern North Received 12 February 2014 China Craton. The sediments in the Upper Jurassic to Lower Cretaceous Tuchengzi Formation in the Received in revised form 30 June 2014 Chengde Basin provide a detrital record of basin dynamics and uplift of the basin margins during that Accepted 11 August 2014 time. We analyzed the sedimentary facies, paleocurrents, and provenance of the Tuchengzi Formation Available online 29 August 2014 in the Chengde Basin for the period of the and shortening in the Yanshan fold-thrust belt. Four sedimentary facies associations have been identified in the Tuchengzi Formation, Keywords: corresponding to proximal fan, mid-fan, distal alluvial fan, and fluvial facies. The transport and distribu- Chengde Basin tion of the Upper Jurassic to Lower Cretaceous sediments in the Chengde Basin was controlled by the Tuchengzi Formation Basin filling faults bounding the basin. Paleocurrent indicators and provenance data of conglomerate clasts reveal that Clast compositions the sediments of the Tuchengzi Formation in the northern part of the Chengde Basin were delivered from Sedimentary facies source regions to the north of the basin. The early sediments of the Tuchengzi Formation in the southern Yanshan fold-thrust belt part of the basin comprise a suite of fluvial deposits, similar to the fluvial sediments in the northern part of the basin, and their paleocurrent data and the compositions of conglomerate clasts also suggest a northern source. However, the subsequent sedimentation in the Tuchengzi Formation in the southern part of the basin changed markedly to proximal fan facies, with sediments being derived from the south of the basin, according to the paleocurrent data and conglomerate clast lithology. The Sandaohe sheet, which is located in the southeast limb of the Chengde syncline, is not a klippe formed as a result of long-distance northward thrusting, but an autochthonous pop-up tectonic wedge generated by N–S shortening during the Early Cretaceous sedimentation of the Tuchengzi Formation. The sedimentation ended before the onset of the Early Cretaceous volcanic eruption recorded by the Formation, which unconformably overlies the Tuchengzi Formation. Ó 2014 Elsevier Ltd. All rights reserved.

1. Introduction occurred during the Late Jurassic and Early Cretaceous (Wong, 1927; Cope et al., 2007). After the North China Craton (NCC) collided with the Mongolian The Chengde Basin is located in the central segment of the YFTB, arc terranes during the late Paleozoic, the northern edge of the NCC with its northern margin bounded by the Fengning-Longhua Fault evolved from a plate margin to an intraplate environment (Davis and its southern margin by the Chengde County Fault (Figs. 1 and et al., 2001). The Yanshan fold-thrust belt (YFTB) is located near 2). A 20-km-wide asymmetric syncline, called the Chengde syn- the northern margin of the North China Craton (Fig. 1), and expe- cline, lies between the Shuangmiao Fault in the central part of rienced at least two major episodes of compressional deformation the basin and the Jiyuqing Fault at the southern margin of the basin during the Mesozoic. The first contraction occurred during the Late (Fig. 2). Although strongly deformed in the Jurassic Yanshanian and Early Jurassic, and the second compression, also movement, the Chengde Basin offers a crucial location for studying known as the ‘‘Yanshanian movement’’ or ‘‘Yanshanian event’’, the context of the tectonic-sedimentary response, because of the relatively complete preservation and good outcrops of Mesozoic sedimentary rocks within the basin. Basin-fill sediments are records of contemporaneous tectonic ⇑ Corresponding author at: No. 11 South Minzudaxue Road, Haidian District, Beijing 100081, China. Tel./fax: +86 (10) 88815007. activities, and can provide constraints not only on paleogeographic E-mail address: [email protected] (J. Liu). conditions, but also on the timing and magnitude of shortening http://dx.doi.org/10.1016/j.jseaes.2014.08.019 1367-9120/Ó 2014 Elsevier Ltd. All rights reserved. 612 J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622

Fig. 1. Geological sketch map of the northern margin of the NCC (modified after Zhang et al., 2007; index figure modified after Davis et al., 2001). WH, Western Hills of Beijing; LP, Luanping Basin, northern ; CD, Chengde Basin, northern Hebei; X, Xiabancheng Basin, northern Hebei; NYZ, Niuyingzi Basin, western ; BPL, Beipiao Basin, western Liaoning. and associated thickening (e.g., Liu et al., 2004, 2012; He et al., and provenance analysis. Four sedimentary facies associations 2007; Cope et al., 2007). Thus, in combination with structural rela- are identified, corresponding to proximal fan, mid-fan, distal allu- tionships and geochronology, sediments can be used to address the vial fan, and fluvial environments. We demonstrate that the Tuc- depositional environments, provenance characteristics, and devel- hengzi sediments in the northern part of the Chengde basin and opment and deformation of the sedimentary basins in the Yanshan the early Tuchengzi sediments in the southern part of the basin belt during the Late Jurassic–Early Cretaceous shortening. Some were transported from source areas to the north of the basin, previous structural and geochronologic studies have interpreted whereas the subsequent Tuchengzi sediments in the southern part the Chengde syncline as representing a folded allochthon that of the basin were derived from the south. In particular, we high- resulted from long-distance north-vergent thrusting with a dis- light that rapid uplift and erosion of the Sandaohe sheet at the placement of at least 40 km (Davis et al., 1998, 2001). In contrast, southern margin of the Chengde syncline provided substantial other studies have provided geometric, kinematic, stratigraphic, amounts of material for the Tuchengzi Formation in the southeast- provenance, and geochronologic evidence that the faults bounding ern Chengde basin. the northern and southern limbs of the Chengde syncline (i.e., the Shuangmiao and Jiyuqing faults) are two separate thrust faults with opposing north and south vergence rather than a single folded 2. Geological background north-directed thrust, and that the sedimentary rocks within the syncline are not allochthonous (e.g., Zhao et al., 2004; Cope et al., 2.1. Geological setting 2007; He et al., 2007; Zhang et al., 2012). Although there is now a consensus that the Chengde syncline is not a nappe, the forma- The northern margin of the NCC, which is located southeast of tion of the Sandaohe sheet, which is located in the southeast limb the Central Asian Orogenic Belt, is divided into two E–W-trending of the Chengde syncline, and its role in the development of the tectonic units by the -Gubeikou Fault (also referred to as Chengde Basin are not well constrained. The Sandaohe sheet is the Shangyi-Gubeikou-Pingquan Fault; HBGMR, 1989). The two dominated by Meso–Neoproterozoic carbonate rocks and is sur- units are named the Inner Mongolia Paleo-Uplift (IMPU) in the rounded by Upper Jurassic Tiaojishan volcanic rocks. Knowledge north and the Yanshan fold-thrust belt (YFTB) in the south of its method of formation is important for better understanding (Fig. 1). The IMPU is characterized by extensive Archean–Protero- the scale of the compressional deformation in the Yanshan fold- zoic high-grade basement rocks that are unconformably overlain thrust belt during the Late Jurassic and Early Cretaceous; that is, by Jurassic–Cretaceous volcanic and sedimentary rocks. The entire whether the Yanshan fold-thrust belt experienced long-distance tectonic province was exhumed during the late to northward thrusting during this interval, as suggested by Davis Early Jurassic (Zhao, 1990; Zhang et al., 2007). et al. (2001), or instead relatively limited N–S shortening. The YFTB consists mainly of a Paleoproterozoic basement, Mes- In this study, we investigate the Upper Jurassic–Lower Creta- oproterozoic sediments, to marine clastic and ceous Tuchengzi Formation across the Chengde Basin from north carbonate platform sediments, middle Carboniferous to Triassic to south, employing detailed sedimentary facies relationships fluvial and deltaic sediments, and Jurassic to Cretaceous (and J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 613

Fig. 2. Geological sketch map of the eastern segment of the YFTB (modified after HBGMR, 1989; Zhang et al., 2009). U–Pb zircon data are from Davis et al. (2001), Liu et al. (2006), Zhang et al. (2004b), and Zhao et al. (2004). younger) volcanic and sedimentary rocks. The maximum thickness marks the southern boundary of the Chengde Basin (Zhang et al., of the Mesoproterozoic and early Paleozoic strata in the YFTB is ca. 2004a). From bottom to top, the hanging wall of the Chengde 11.5 km (HBGMR, 1989), but these units are almost entirely absent County Fault consists of: (1) Mesoproterozoic carbonate rocks of from the IMPU, except for some Mesoproterozoic sedimentary the Jixian Group, which are buff-colored, thinly bedded to stromat- rocks that form a narrow belt along the Fengning-Longhua Fault olitic dolomites containing variable amounts of chert; (2) thinly (Fig. 1). bedded, white, laminated limestones interbedded with black shales of the Neoproterozoic Qingbaikou Group, within which 2.2. Characteristics of thrust faults in the Chengde Basin diabase sills (up to ca. 50 m thick) are present; (3) Paleozoic (Cambrian–Ordovician) carbonates consisting of blue to blue- The major thrust faults in the Chengde area are generally east– gray, mottled or banded limestones and sparse, dark-brown west trending. The most important fault structures in the Chengde dolomites; and (4) volcanic rocks of the Upper Jurassic Tiaojishan Basin (Fig. 1) are the Fengning-Longhua Fault (FL F.) to the north Formation. and the Chengde County Fault (CC F.) to the south, but several sec- The Shuangmiao Fault (SM F.) in the central part of the Chengde ond-order faults have also been mapped (Davis et al., 2001; Basin and the Jiyuqing Fault (JYQ F.) at the southern margin of the HBGMR, 1989; Fig. 2). basin mark respectively the northern and southern boundaries of The Paleoproterozoic Fengning-Longhua Fault (Fig. 2) is the the Chengde syncline (Fig. 2), an asymmetric syncline that is northern boundary of the Yanshan belt (Fig. 1; HBGMR, 1989). 20 km wide from north to south. The Shuangmiao Fault (Fig. 3)is The footwall consists of Archean rocks, which are unconformably a south-dipping thrust. A narrow belt of the Proterozoic Changch- overlain by Upper Jurassic to Lower Cretaceous conglomerates eng Group crops out on the hanging wall of the fault. The footwall and Lower Cretaceous volcanic rocks (HBGMR, 1989). This fault contains conglomerates of the Upper Jurassic–Lower Cretaceous experienced intense tectonic activity during the late Paleozoic Tuchengzi Formation, which is folded at some places close to the and Mesozoic. It now forms the northern boundary of the Jurassic fault plane. Slickensides, together with the folded structure, Chengde Basin, and exerted a strong control on basin development indicate northward movement of the Shuangmiao Fault. The during the Late Jurassic and Early Cretaceous (HBGMR, 1989; Liu Jiyuqing Fault (JYQ F., Fig. 3) is a steeply north-dipping thrust, with et al., 2004; He et al., 2007). the Proterozoic Changcheng Group on the hanging wall and the The Chengde County Fault (Figs. 2 and 3) experienced tectonic Upper Jurassic volcanic rocks of the on the activity during the Late Jurassic and Early Cretaceous and this fault footwall. 614 J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622

Fig. 3. Geological sketch map of Chengde County, northern Hebei Province (HBGMR (1976); authors’ data, see Fig. 2). Key: 1, Quaternary sediments; 2, Lower Cretaceous volcanic and sedimentary rocks; 3, fine sandstone; 4, siltstone; 5, conglomerate and pebbly sandstone; 6, conglomerate; 7, volcanic rocks; 8, Upper Jurassic Jiulongshan Formation; 9, Middle Jurassic Xiahuayuan Formation; 10, Middle Jurassic Nandaling Formation; 11, Lower Jurassic Xingshikou Formation; 12, Middle Triassic Ermaying Formation; 13, Lower Triassic Liujiagou Formation; 14, Ordovician sedimentary rocks; 15, Cambrian sedimentary rocks; 16, Qingbaikou system; 17, Jixianian system; 18, Changchengian system; 19, Archean metamorphic rocks; 20, Early Cretaceous granite; 21, Late Jurassic granite; 22, paraconformity; 23, unconformity; 24, anticline; 25, syncline; 26, thrust fault; 27, normal fault; 28, strike-slip fault and fault with uncertain kinematics; 29, attitude and inverted attitude; 30, paleocurrent data; 31, U–Pb zircon ages; 32, 40Ar–39Ar hornblende ages. U–Pb zircon and 40Ar–39Ar data are from: (1) Davis et al. (2001); (2) Cope et al. (2007); (3) Zhao et al. (2004); (4) Niu et al. (2004); (5) Davis (2005); and (6) Liu et al. (2006). F.A.: Facies Association.

The steeply south-dipping Hualiangou-Hedong Fault (HH F., 2.3. Age of the Tuchengzi Formation in sedimentary basins of the Fig. 3) marks the northern boundary of the lenticular Sandaohe central YFTB sheet (Zhao et al., 2004), the southern boundary of which is the Jiyuqing Fault. The footwall of the Hualiangou-Hedong Fault con- The Tuchengzi Formation is widely distributed and trends E–W sists of Upper Jurassic volcanic rocks of the Tiaojishan Formation, in the northern part of North China. The Tuchengzi Formation rests and the hanging wall is made up of Proterozoic chert-bearing car- unconformably on pre-Mesozoic units at Chicheng in northern bonate rocks of the Jixian Group. Our field observations show that a Hebei Province, but elsewhere it commonly overlies Upper Jurassic limited area of the Tiaojishan volcanic rocks lie unconformably on rocks known as the Tiaojishan (Lanqi) Formation, which is com- Proterozoic carbonate rocks within the Sandaohe sheet (Fig. 3). posed predominantly of andesitic, trachyandesitic, and pyroclastic J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 615

Fig. 4. Upper Jurassic–Lower Cretaceous stratigraphy of the YFTB, showing the units discussed in the text. Key: 1, coal measures; 2, medium-coarse sandstone; 3, conglomerate and pebbly sandstone; 4, conglomerate and tuffaceous conglomerate; 5, tuffaceous sandstone; 6, crystal tuff; 7, dacite; 8, rhyolite; 9, andesite and andesite porphyry; 10, andesitic breccia and andesitic conglomerate; 11, trachyandesite; 12, andesite-basalt; 13, basalt; 14, U–Pb zircon ages; 15, 40Ar–39Ar hornblende ages; 16, 40 39 40 39 40 39 Ar– Ar biotite ages; 17, Ar– Ar feldspar age; 18, U–Pb zircon or Ar– Ar data; 19, paraconformity; 20, unconformity; J3–K1tch, Upper Jurassic–Lower Cretaceous

Tuchengzi Formation; J3t, Upper Jurassic Tiaojishan Formation; J3j, Upper Jurassic Jiulongshan Formation; J2h, Middle Jurassic Haifanggou Formation; J2g, Middle Jurassic 40 39 Guojiadian Formation; T2e, Middle Triassic Ermaying Formation. U–Pb zircon and Ar– Ar data are from: (1) Davis et al. (2001); (2) Li et al. (2001); (3) Swisher et al. (2002); (4) Cope et al. (2007); (5) Peng et al. (2003); (6) Zhao et al. (2004); (7) Gao et al. (2004); (8) Zhang et al. (2005a); (9) Zhang et al. (2005b); (10) Yuan et al. (2005); (11) Davis (2005); (12) Yang & Li (2005); (13) Liu et al. (2006); (14) Hu et al. (2007); and (15) Zhang et al. (2012).

rocks. The contact relationships between the Tuchengzi Formation overlying Tuchengzi Formation. Therefore, the age of the top of and the underlying Tiaojishan Formation are generally described as the Tiaojishan Formation is the preferred basis for constraining disconformable or conformable (HBGMR, 1989; Xu et al., 2012; the age of the base of the Tuchengzi Formation. Fig. 4 shows that Fig. 2). the youngest zircon U–Pb age for the top of the Tiaojishan Forma- The Chengde Basin contains volcanic and volcaniclastic strata tion is ca. 153 Ma (Cope, 2003; Liu et al., 2006), consistent with ca. 900 m thick, preserved only in the southern and westernmost the zircon age of 152 ± 3 Ma for the tuff layer near the base of portions of the basin, and about 2000 m of fluvial and alluvial the Tuchengzi Formation (Cope, 2003). The Tuchengzi Formation conglomerates, sandstones, and shales assigned to the Tuchengzi is overlain, sometimes unconformably, by silicic volcanic rocks Formation (HBGMR, 1989). These are underlain by andesitic vol- of the Lower Cretaceous Zhangjiakou Formation. These volcanic canic rocks assigned to the Tiaojishan Formation, which yield rocks consist mainly of tuffs with intercalated sediments; SHRIMP U–Pb ages ranging from approximately 160 to 157 Ma (Zhao U–Pb zircon dating in Jiguanshan, Chengde, northern Hebei, has et al., 2004; Liu et al., 2006). These volcanic rocks are also found yielded an age of 135 ± 1 Ma (Zhao et al., 2004), slightly younger farther to the west and east: in the western hills of Beijing, in the than the youngest zircon U–Pb age of 139 ± 1 Ma for a tuff layer Luanping Basin in northern Hebei Province, and in the Niuyingzi near the top of the Tuchengzi Formation in the northern limb and Beipiao basins in western Liaoning Province (Fig. 4). Field of the basin (see Fig. 1 of Zhang et al., 2012; Fig. 4). These dates observations indicate that there was no significant break in depo- thus constrain the age span of the Tuchengzi Formation to 153– sition between the Upper Jurassic Tiaojishan Formation and the 135 Ma. 616 J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622

Fig. 5. Measured stratigraphic sections of the Tuchengzi Formation in the Chengde County area, Chengde Basin, showing paleocurrent data and clast provenance data as recorded in (a) section A–A0, (b) section B–B0, and (c) section C–C0.

3. Sedimentary facies, provenance, and unroofing as recorded in in Fig. 5. Measurements of the Tuchengzi Formation from the the Tuchengzi Formation, Chengde Basin northern part of the basin reveal no upsection shift in sediment dispersal patterns and consistently show dominantly southward 3.1. Paleocurrent data paleocurrents (Figs. 3 and 5a), suggesting that these sediments were transported from the north. However, upsection paleocur- Paleocurrent indicators were measured across the Chengde rents measured from the southern limb of the Chengde syncline Basin from north to south. Paleocurrent directions in the Tuchengzi shift from south-directed paleoflows in the lower Tuchengzi Formation were determined from the largest flat gravel clasts in Formation to north-directed paleoflows in the upper Tuchengzi gravelly sandstones containing imbricate structures, layers with Formation (Figs. 3 and 5b and c). Accordingly, the source region tabular cross-bedding, and other sedimentary structures. A total of the Tuchengzi sediments in the southern part of the basin is of 800 measurements were obtained at 26 sites. The upsection suggested to have changed from a northern source to a southern sediment dispersal patterns in the Tuchengzi Formation are shown one, with the latter being the major source. J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 617

Table 1 Facies codes, sedimentary structures, and interpretations of the Fenghuoshan and Yaxicuo groups, modified from Miall (1978).

Facies Lithofacies Sedimentary structures Interpretation codes Dm Diamictite Massive Mudflows Gmm Matrix-supported conglomerate Massive Debris flows and mudflows Gcm Clast-supported conglomerate Massive Turbulent flow as the bottom load in high-energy gravel channels Gh Clast-supported conglomerate Crude cross-beds and Ancient piling up imbrication Gl Thin-stratified or lens-shaped, matrix or grain supported Grading or none Minor channel fills gravel Gt Clast-supported conglomerate. Trough cross-beds High-energy stream-channel flow St Sand, medium to coarse, pebbly Trough crossbeds Dunes Sp Sand, medium to coarse, may be pebbly Planar crossbeds Linguoid bars Sm Sand, very fine to coase, may be pebbly. Parallel bedding, steaming Planar bed flow lineation Sh Sand, very fine to coase Horizontal lamination Lower flow regime Fm Mud, silt Massive, desiccation cracks Overbank or lake

Fig. 6. Vertical and lateral arrangement of facies associations recorded in the Upper Jurassic–Lower Cretaceous Tuchengzi Formation, Chengde Basin. Proximal fan facies associations a recorded in section B–B0 and C–C0; mid-fan facies associations b recorded in section A–A0; distal-fan facies association c recorded in section A–A0; fluvial facies association d recorded in section A–A0 and B–B0, see Fig. 3.

3.2. Sedimentary facies analysis We identified four different facies associations on the basis of lithology, sedimentary structures, and architecture. The four iden- We employed the facies classification proposed by Miall (1978, tified lithofacies associations can be matched with proximal fan, 1996), in which successions containing at least 50% gravel are mid-fan, distal fan, and fluvial environments (Figs. 3 and 6), and denoted G facies, and sandy and sandy-clayey facies are defined are described in turn below. as S and F facies, respectively. Small letters following the capital letter indicate the textural and structural characteristics of each 3.2.1. Facies association 1: proximal fan facies. Some modifications were necessary to include the facies This facies association is restricted to the southern limb of the varieties identified in the area, such as the introduction of the Chengde syncline (Fig. 3), where it is characterized by conglomer- Dm facies (massive diamictites). Table 1 lists the lithofacies found ates that thicken and coarsen to the north. This facies association in the Chengde area and their respective codes. consists of the Dm (massive diamictite), Gmm (massive, matrix- The Tuchengzi Formation in the Chengde Basin consists mainly supported conglomerate), Gcm (massive, clast-supported con- of a set of fluvial and alluvial coarse-grained clastic sediments, and glomerate), and, in lower proportions, Gh (crude, cross-bedded, the distribution of every sedimentary facies in the formation is eas- clast-supported conglomerate) and Fm (massive mudstone) facies ily observed and measured. (Table 1; Fig. 6a). We measured seven stratigraphic sections within the Tuchengzi Intercalations are observed between the Dm and Gmm facies Formation and four N–S cross-sections through the Chengde Basin, and between the Dm and Gcm facies. The Dm and Gcm facies form including section A–A0 in the northern part of the basin, and sec- meter-scale (2–10 m) packages that predominate compared with tions B–B0 and C–C0, in the southern limb of the Chengde syncline. the other facies. The Fm facies occurs in the form of layers 1–2 m 618 J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622

Fig. 7. Photographs of structural relationships and clast lithologies in the Chengde Basin. (a) Gneiss and granite clasts sourced from Archean–Paleoproterozoic high-grade basement rocks. (b) ‘Bamboo carbonate’ clast, typical of lithologies of the Cambrian strata. (c) Volcanic rocks of the Tiaojishan Formation commonly overlie Proterozoic strata of the Sandaohe sheet (see Fig. 2). (d) Volcanic rock clasts, typical of the lithologies of the Tiaojishan Formation proximal to the ‘Sandaohe sheet’. VR, volcanic rocks; Gn, gneiss; Gr, granite; Qz, quartzite. thick intercalated among the Dm, Gmm, and Gcm facies, as well as 3.2.2. Facies association 2: mid-fan millimeter- to centimeter-thick lenses (up to 20 cm) interfingered The mid-fan facies association is represented throughout sec- between Dm layers. tion A–A0, and the facies crops out from west to east in the Tangji- Facies Gmm and Dm are interpreted as having been formed awan to Liugou areas in the northern limb of the Chengde Basin from debris flows and mudflows; the difference between them is (Fig. 3). The mid-fan facies association is represented by a thick the percentage of clay, which is markedly higher in the latter. succession of sandstones with intercalations of conglomerate and Transport occurred by viscous flow that deposited clay together mudstone, and the association is a mix of Gcm, Sm, Sh, and Fm with grains of variable size, resulting in poorly sorted deposits. facies (Table 1; Fig. 6b). The Gcm facies is found only close to the Although they typically represent isotropic deposits, normal or northern margin of the basin, is limited in thickness, and is inter- inverse grading and clast alignment can be found where a flow preted as debris flows. was less viscous (Bull, 1972), as observed for the Dm facies. The facies association Sm (massive, fine to very coarse, gener- The Gcm facies also can be formed by debris flow when fine ally pebbly sandstone) and Sh (laminated fine to medium sand- sediments are absent in the source area, but the possibility that stone), is generally found in the transition to the Fm facies this facies was deposited through turbulent flow as the bottom (massive mudstone) in fining-upward sequences. The transition load in high-energy gravel channels should not be ignored (Miall, from Sm to Fm occurs in strata with thicknesses of approximately 1996). 1–2 m, whereas the transition from Sh to Fm occurs at scales of The Gh facies forms lenticular layers 30–50 cm thick. Gcm millimeters to centimeters (not exceeding 30 cm). The association facies associated with Gh facies are often the only traces of an (Sm, Sh, and Fm) can be interpreted as channel overflow deposits ancient accumulation. The lenticular geometry of the strata, the formed during flood periods, when the water carrying debris over- presence of a planar-parallel stratification, and clast imbrication flowed from the channels and deposited material in lobate sheets. indicate the high energy of the aqueous flow responsible for its for- The high-energy, nonchanneled aqueous flow deposited stratified mation (Nilsen, 1982). These facies may have been deposited at the or massive sand; with the loss of energy, the flow ceased, and its bottom of high-energy, straight or braided channels located in the suspension load settled out as clayey layers. The lower contact middle or distal alluvial fan. These channels can often be between layers is often erosive, with deformation of the clayey obstructed by debris or mud flow when tectonic pulses reoccur. level caused by the sandy flow. These deposits can be found in The origin of the Fm facies may be related to the formation of the intermediate portion of an alluvial fan system, where the slope water bodies where fine sediment settling occurred. These features is shallower and coalescence between fans occurs. are common in the case of the interfingering of depositional lobes and the formation of small depressions subsequently filled by 3.2.3. Facies association 3: distal fan other flows. The distal-fan association consists of facies Gt (cross-bedded, These features, combined with the fact these rocks occur only in clast-supported conglomerate), St (cross-bedded, fine to very isolated patches close to the southern margin of the basin, and in coarse, sometimes pebbly sandstone), and Sh (laminated, very fine contact with volcanic rocks, suggest deposition in the proximal to medium sandstone) (Table 1; Fig. 6c), and it forms the second part of a series of coalescing alluvial fans. segment of the Tuchengzi Formation in section A–A0 (Fig. 3), where J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 619

Fig. 8. Schematic model of the development of the Chengde Basin. See Section 4.2 for details. it is around 800 m thick. These facies occur intercalated in the form The floodplain deposits consist of violet-colored mudstones of lenticular layers with an erosive lower contact, and range in with intercalated thin or muddy siltstone. These deposits may con- thickness from 0.5 to 2 m. The presence of trough cross-beds in this tain the lithofacies association Sh and Fm. Individual muddy silt- association indicates high-energy stream-channel flow. These stone beds are commonly 0.5–1 m thick, but mudstone beds may characteristics might suggest the existence of a distal fluvial be more than 4 m thick. Based on the depositional style, these bed- system terminal to the alluvial fans. load-dominated fluvial deposits are interpreted to have formed in a braided-river system (Miall, 1996). 3.2.4. Facies association 4: fluvial The fluvial association is characterized by sandstones and 3.3. Temporal changes in the gravel components conglomerates that fine and thin upwards with normal graded bedding, and mudstones. It contains channel and overbank The composition of gravels and sandstones in a basin is an subfacies that are found in the upper part of section A–A0 and the important indicator of the uplift and erosional history of moun- bottom part of section B–B0 (Fig. 3). The fluvial association includes tains at the margins of that basin (Hendrix et al., 1996; Hendrix, some subfacies of longitudinal sand bars, bedform lag deposits, and 2000). The sedimentary rocks of the Tuchengzi Formation in the floodplain deposits. Chengde Basin are dominated by gravels. At each site investigated, The longitudinal sand bars consist of medium to thick beds that nearly every gravel clast in a specified area of 2 m2 was identified; are fine- to coarse-grained, characterized by the lithofacies associ- the number of clasts counted was typically more than 80–100. We ation St and Sp (Table 1, Fig. 6d). The sand bars are usually interca- compiled three stratigraphic sections (Fig. 5) of the Tuchengzi For- lated with thin mudstones, indicating sedimentary cycles with mation to show the upward temporal changes in clast composition normal graded bedding, and a single sand-bar sedimentary cycle and abundance. is typically 0.5–1.0 m thick. This association could represent sand Fig. 5a shows the conglomerate compositions of the Tuchengzi bars that moved downstream or beveled a main-stream channel. Formation in the northern limb of the basin. The conglomerate The bedform lag deposits consist of graded conglomerates and clasts within this section of the Tuchengzi Formation are mainly sandstones with a lithofacies association of Gl and Sp (Table 1, volcanic rocks with subordinate amounts of granite and gneiss Fig. 6d). These deposits commonly cover scour surfaces, and they (Figs. 5a and 7a). The granite and gneiss clasts are comparable to typically grade upwards into longitudinal sand bars. The conglom- the Archean basement rocks and Paleozoic granites that lie north erates are stratified or lens shaped and grain supported, and the of the Fengning-Longhua Fault (Figs. 1 and 2). Thus, the Tuchengzi clasts consist of granite, volcanic rock, and sandstone. Formation in the northern Chengde Basin was most likely derived 620 J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 from the ancient basement with a Jurassic volcanic cover north of This inferred south-dipping paleoslope is also consistent with the Fengning-Longhua Fault. This inference is in agreement with the N–S distribution of sedimentary facies association across the the numerous southward paleocurrent indicators measured basin from mid-fan facies, through distal fan facies, to fluvial facies throughout the northern Chengde Basin (Fig. 3). Fig. 5b shows (Fig. 3). The lack of proximal fan facies at the northern margin was the temporal changes in the conglomerate compositions of the probably because the relief and slope to the north of the basin were Tuchengzi Formation in the southern part of the basin. In the bot- not sufficiently steep. tom section, the conglomerate clasts consist mainly of volcanic The paleogeography of the southern margin of the basin experi- rocks (50%) with subordinate amounts of granite (25%) and enced a significant change after deposition of the lower Tuchengzi gneiss (25%), similar to the clasts in the Tuchengzi Formation in sediments in the southern limb of the Chengde syncline. The the northern part of the basin. In combination with the southward coarse, poorly sorted conglomerate clasts in the upper Tuchengzi paleocurrent data (Figs. 3 and 5b), these early Tuchengzi sediments Formation in the southern limb reflect a proximal fan facies in the southern Chengde basin are considered to have had the same (Fig. 3). In combination with the northward paleocurrents recov- northern source as the Tuchengzi sediments in the northern part of ered from the clasts and clast lithology (Figs. 3 and 5b and c), this the basin. proximal fan facies suggests a southern source proximal to the In the dominant, upper section (Fig. 5b), however, the clast active southern margin of the basin. Uplift and erosion of the hang- lithology changes drastically. The clasts consist mainly of volcanic ing wall of the Chengde County Fault to the south of the basin and rocks and banded (or bamboo) limestones (25–95% and 0–35%, of the Sandaohe sheet at the southern basin margin were most respectively). Minor clast components include blue dolomite and likely responsible for the coarse sediment influx northward into chert clasts (5–20% and 5–25%, respectively). The proportion of the southern part of the basin. volcanic clasts decreases markedly upward through the section. Conversely, the proportions of banded limestone and blue dolo- 4.2. Implications for the development of the Chengde Basin mite clasts increase upward, and can clearly be linked to the Cam- brian–Ordovician carbonate rocks present only in the hanging wall The sediments of the Upper Jurassic–Lower Cretaceous Tuc- of the Chengde County Fault to the south of the basin. Similarly, the hengzi Formation in the Chengde basin, consisting of conglomer- percentage of chert clasts derived from the Jixian Group increases ates, sandstones, shales, and minor volcanic tuffs, provide a upward in the succession. These temporal trends reflect progres- detrital record of the basin dynamics and uplift of the basin margin sive unroofing and erosion of the Upper Jurassic volcanic rocks of during the Late Jurassic and Early Cretaceous. Based on the sedi- the Tiaojishan Formation followed by the Paleozoic and Mesopro- mentary evidence presented in this study, we propose the follow- terozoic carbonate rocks to the south of the basin (Figs. 5b and 7b). ing scenario for the Late Jurassic and Early Cretaceous Also in the southern limb of the Chengde syncline, we measured development of the Chengde Basin. another section in the Tuchengzi Formation north of the Sandaohe During the early Late Jurassic, multiple eruptions of extensive sheet. As shown in Figs. 5c and 7d, the clasts in this section consist intermediate–felsic volcanic rocks occurred in the Chengde area, mainly of volcanic rocks (95–100%) with small amounts of chert forming the Tiaojishan Formation (Fig. 8a). These Upper Jurassic (0–5%). We interpret that the volcanic clasts were derived from Tiaojishan volcanic rocks (ca. 160–153 Ma) unconformably cov- the Upper Jurassic Tiaojishan Formation volcanic cover within ered the older Jurassic strata (198–180 Ma, Davis et al., 2001; Liu the adjacent Sandaohe sheet. The chert clasts were likely derived et al., 2012) that were deposited prior to the eruptions, as well as from the Jixian Group exposed in the Sandaohe sheet as a result Proterozoic–Paleozoic carbonate rocks and Archean basement. of unroofing of the sheet. The dominance of coarse volcanic clasts Following the sedimentation of the Tiaojishan volcanic strata, a through this section, in combination with north-directed paleocur- series of nearly E–W trending thrust faults bounding the Chengde rents and the remnants of the Tiaojishan Formation volcanic cover basin were strongly activated as a result of intracontinental N–S (Figs. 3, 5c, and 7d), indicates a very proximal derivation from the tectonic compression. These thrusts include the Fengning-Longhua nearby Sandaohe sheet, which experienced rapid uplift and signif- and Damiao faults to the north, and the Chengde County, Jiyuqing, icant erosion of the Tiaojishan volcanic cover. The absence of Cam- and Hualiangou-Hedong faults to the south. sediments of the brian bamboo carbonate clasts together with the rare chert clasts Upper Jurassic–Lower Cretaceous Tuchengzi Formation (153– suggests that the rapid uplift of the Sandaohe sheet might have 139 Ma; Figs. 3 and 8b) in the Chengde Basin recorded the uplift acted as a significant topographic barrier preventing north-vergent and erosion of the basin margins during this time. In the northern delivery of carbonate sediments from the more distal hanging wall Chengde Basin, the sediments in the Tuchengzi Formation were of the Chengde County Fault into the southeastern Chengde Basin. dominantly sourced from the region north of the Fengning-Long- hua Fault. Jurassic volcanic rocks, Paleozoic granites, and Precam- brian basement gneisses were eroded from the hanging wall of 4. Discussion the Fengning-Longhua Fault and transported southward into the Chengde Basin, as demonstrated by the south-directed paleocur- 4.1. Basin paleogeography rents and comparable conglomerate clasts recorded in the Tuc- hengzi Formation throughout the northern part of the basin. The The prevailing southward paleocurrent data and north-derived Shuangmiao Fault within the basin was not active during this per- basement clasts present in the Tuchengzi Formation in the iod and made little contribution to the deposition of the Tuchengzi northern part of the Chengde basin (Figs. 3 and 5a) suggest for Formation, because the Tuchengzi Formation is cut by this fault these Tuchengzi sediments a primary source region to the north and the lithofacies and conglomerate clast lithology of the Tuc- of the basin drained by southward-flowing rivers. North-derived hengzi Formation are well matched between its hanging wall and sediments in the lower Tuchengzi Formation in the southern limb footwall (e.g., Cope et al., 2007; He et al., 2007; this study). of the Chengde syncline (Figs. 3 and 5b) further suggests that those During the late Tuchengzi period (ca. 139–135 Ma) prior to the southward-flowing rivers, which dominated in the northern part of Early Cretaceous Zhangjiakou Formation volcanic eruptions, the the basin, had advanced and delivered sediments to the southern Shuangmiao Fault was activated and thrust northward (Fig. 8c), part of the basin. Thus, a southward-inclined paleoslope is implied indicating another N–S contraction that was probably much for the vast majority of the basin, with a depocenter probably weaker than the shortening during the sedimentation of the Tuc- located proximal to its southern margin. hengzi Formation. The folded Tuchengzi Formation in the footwall J. Liu et al. / Journal of Asian Earth Sciences 114 (2015) 611–622 621 of the Shuangmiao Fault (see Section 2.2) may be related to this filled with continental red beds (Davis et al., 1996, 2002; Meng, northward thrusting of the fault. 2003; Liu et al., 2005; Charles et al., 2010). Coevally, the Tuchengzi sediments in the southern part of the Our new sedimentological data are in agreement with the inter- basin (i.e., the southern limb of the Chengde syncline), in contrast pretation that the northern and southern basin-bounding faults to those in the northern basin, were derived from source areas (i.e., the Shuangmiao and Jiyuqing faults) are two separate thrust south of the basin. Progressive unroofing of the Upper Jurassic vol- faults that had opposing north and south vergence (e.g., Zhang canic rocks of the Tiaojishan Formation and the Paleozoic and Mes- et al., 2012) during the development of the Chengde Basin, but oproterozoic carbonate rocks from the hanging wall of the Chengde are inconsistent with the interpretation that the basin was devel- County Fault generated a significant sediment influx northward oped from folding of an allochthon that resulted from long-dis- into the southern part of the basin, and formed a relatively tance north-vergent thrusting as suggested by Davis et al. (1998, restricted proximal fan facies (Facies Association 1; Fig. 3) overly- 2001). ing the early Tuchengzi sediments of fluvial facies derived from the north. In the southeastern limb of the Chengde syncline, opposite- directed thrusting of the Hualiangou-Hedong and Jiyuqing faults 5. Conclusions during the N–S shortening resulted in rapid uplift of the Sandaohe sheet and formed a steep pop-up tectonic wedge (Fig. 8c), which We analyzed the sedimentary facies, paleocurrents, and prove- was originally covered by the Upper Jurassic Tiaojishan volcanic nance of the Tuchengzi Formation in the Chengde Basin for the per- rocks. Significant erosion of the Tiaojishan Formation volcanic iod of the Late Jurassic and Early Cretaceous shortening in the cover atop the Sandaohe sheet produced an influx of volcanic Yanshan fold-thrust belt. Our main conclusions are as follows. materials that were transported northward and rapidly deposited Four sedimentary facies associations have been identified in the in the southeastern limb of the Chengde syncline, forming a Tuchengzi Formation, corresponding to proximal fan, mid-fan, dis- restricted proximal fan facies (Facies Association 1; Fig. 3) of the tal alluvial fan, and fluvial facies. The transport and distribution of Tuchengzi Formation in close proximity to the Sandaohe sheet. the Upper Jurassic–Lower Cretaceous sediments in the Chengde This process is reflected well in the Tuchengzi Formation north of Basin were controlled by the faults bounding the basin. the Sandaohe sheet, as indicated by north-vergent paleocurrent Paleocurrents and provenance data of conglomerate clasts indicators and the dominance (almost 100%) of coarse volcanic reveal that the sediments of the Tuchengzi Formation in the north- clasts within the strata (Figs. 3, 5c, and 7d). The absence of Cam- ern and southern parts of the Chengde basin were transported brian bamboo carbonate clasts together with the presence of rare from source areas to the north and south of the basin, respectively. chert clasts indicates that the uplifted Sandaohe sheet acted as a The Tuchengzi Formation in the northern part of the basin was drainage barrier that effectively shut off sediment influx sourced derived from erosion of the hanging wall of the Fengning-Longhua from the more distal hanging wall of the Chengde County Fault. Fault. The Tuchengzi Formation in the southern part of the basin Thus, the source region of the Tuchengzi Formation north of the was derived partly from the unroofing of the hanging wall of the Sandaohe sheet is different from that of the strata elsewhere in Chengde County Fault; another important sediment contribution the southern part of the basin. The possibility that the Sandaohe was derived from the rapid uplift and erosion of the Sandaohe sheet is a klippe resulting from long-distance north-vergent thrust- sheet, which is located in the southeastern limb of the Chengde ing, as inferred from the interpretation of Davis et al. (1998, 2001), syncline. is ruled out in our proposed scenario. If the Sandaohe sheet were a The Sandaohe sheet is not a klippe resulting from long-distance klippe, the associated thrust (the ‘‘Chengde Thrust’’ in previous north-vergent thrusting, but an autochthonous pop-up wedge gen- studies) would have overlain the Cambrian–Ordovician carbonate erated by N–S shortening during the sedimentation of the Lower strata in the hanging wall of the Chengde County Fault (see Fig. 6 Cretaceous Tuchengzi Formation. in Davis et al., 2001), precluding erosion of those Paleozoic carbon- ate rocks and their transportation into the southern part of the Acknowledgments Chengde Basin, contrary to the sedimentological evidence of the present study. The Sandaohe sheet is therefore an autochthonous This research was financially supported by the ‘Deep Explora- pop-up formed during sedimentation of the Lower Cretaceous Tuc- tion Technology and Experimentation’ Program of China (SinoP- hengzi Formation. robe-08-01-03) and the National Basic Research Program of The north of the basin formed earlier (153–139 Ma), the fault China (Grant 2006CB403501 to Y. Zhao). (FL F.) along the northern margin of the basin may control the sed- imentary of the Tuchengzi Formation in the early stage. After the References sedimentary in the north (>139 Ma), the Sandaohe Sheet at the southern margin of the basin began to uplift quickly and the fault Bull, W.B., 1972. Recognition of alluvial fan deposits in the stratigraphic record. In: (e.g. CC F.) bounding the basin in the south became strongly active, Rigby, J.K., Hamblin, W.K. (Eds.), Recognition of ancient sedimentary which resulted in the formation of the matrix strata covering the environments. 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