Soft-sediment deformation structures in the Cretaceous Zhucheng depression, Shandong Province, East China; their character, deformation timing and tectonic implications

Accepted Manuscript Soft-sediment deformation structures in the Cretaceous Zhucheng Depression, Shandong Province, East China; their character, deformation timing and tectonic implications Bizhu He, Xiufu Qiao, Yingli Zhang, Hongshui Tian, Zhihui Cai, Shuqing Chen, Yanxia Zhang PII: DOI: Reference:

S1367-9120(14)00570-7 http://dx.doi.org/10.1016/j.jseaes.2014.12.005 JAES 2201

To appear in:

Journal of Asian Earth Sciences

Received Date: Revised Date: Accepted Date:

2 April 2013 25 November 2014 15 December 2014

Please cite this article as: He, B., Qiao, X., Zhang, Y., Tian, H., Cai, Z., Chen, S., Zhang, Y., Soft-sediment deformation structures in the Cretaceous Zhucheng Depression, Shandong Province, East China; their character, deformation timing and tectonic implications, Journal of Asian Earth Sciences (2014), doi: http://dx.doi.org/ 10.1016/j.jseaes.2014.12.005

This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

Soft-sediment deformation structures in the Cretaceous Zhucheng Depression, Shandong Province, East China; their character, deformation timing and tectonic implications

Bizhu Hea*, Xiufu Qiaoa, Yingli Zhangb, Hongshui Tianc, Zhihui Caia, Shuqing Chendand Yanxia Zhang

a

State Key Laboratory of Continental Tectonics and Dynamics, Institute of Geology, Chinese Academy of Geological Sciences, Beijing, China, 100037

b

Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing, China, 100037

c

Shandong Construction University, Jinan, Shandong, China, 250014

d

Dinosaur National Geopark, Zhucheng, Shandong, China, 262200

*Corresponding author: E-mail: [email protected]; [email protected] (Bizhu He)

Abstract Various plastic and brittle soft-sediment deformation structures (SSDS) are recognized in Cretaceous sedimentary rocks of the Zhucheng depression, East China record important information on the different sediment characteristics, depositional settings and tectonic movements involved in their formation. The recognized SSDS include undulate folds, moundand-sag structures, diapirs, convolute features and a seismically induced unconformity. The Lower Cretaceous sedimentary rocks are fine grained, lacustrine deposits, whereas those of the Upper Cretaceous are coarse-grained sandstones and conglomerates formed in an alluvial fan or flood-plain setting. These SSDS with coarse-grained rocks are characterized by fault grading, load cast structures, ball and pillow structures and plunged sediment mixture structures. We propose that the SSDS was triggered by paleo-earthquakes. Alternating deformed and undeformed layers suggest frequent and repeated seismic activity. Stratigraphic correlations, the evaluation of magmatic events and the youngest detrital zircon ages indicate that the deformational events occurred mainly in the Early Cretaceous between 118 Ma to 105 Ma, and in the Late Cretaceous at approximately 100 Ma. Numerous giant hadrosaurid fossil skeletons have been found in the Upper Cretaceous Wangshi Group, and unusual and abundant dinosaur tracks are preserved in the Lower Cretaceous Yangzhuang Formation of the Laiyang Group. The zones of widespread SSDS closely underlie and overlie the dinosaur fossil-bearing strata. The depositional setting changed in response to multiple paleoseismic events and regional tectonic movements. After many paleoearthquakes and environmental changes in the Early Cretaceous, many dinosaurs appear to have migrated, based on the presence of many tracks with a similar orientation in lacustrine sedimentary rocks. In the Late Cretaceous strata,

large-scale dinosaur fossil layers are associated with paleo-earthquake records, suggesting that the dinosaur fossil burial may be associated with large-scale debris flows triggered by frequent earthquakes. Based on regional tectonic setting, the distribution of SSDS and the predicted paleo-earthquake magnitudes, the seismogenic fault may have been the Wulian Fault.

Key words Soft-sediment deformation structures, deformed time, seismites, dinosaur fossils, Cretaceous, Zhucheng depression, east China

1 Introduction SSDS are features produced when deformation occurs in unconsolidated sediment, typically close to the surface, during or shortly after deposition and before significant

diagenesis (Owen, 1987; Qiao et al., 2006; Owen et al., 2011). Because many processes can produce SSDS, such as tectonic activity, glacier-related deposition, gravity-driven massmovements, sediment mobilization in overpressured and collapsing environments, it can be difficult to determine the exact cause of any given feature. Many things, such as the nature of the driving force, the sediment rheology, deformation mechanism and timing of deformation relative to sedimentation, can affect the final morphology and deformation style of softsediment structures (Obermeier, 1996; Moretti, 1999; Qiao et al., 2006; Owen et al., 2011). Driving forces include gravity acting on slopes, unequal loading, reverse density gradients, shear forces, and biological and chemical agents (Owen et al., 2011). Most SSDS are produced by inputs of kinetic energy from outside the deposystem (Leeder, 1987). Seismic activity with a magnitude of 5 or greater, related to episodic fault motion, is considered the most common trigger, leading to liquefaction of unconsolidated sediments (Allen and Banks, 1972; Allen, 1986; Galli, 2000; Santos et al., 2012). Seismites (proposed by Seilacher, 1969) is the term applied to SSDS produced by earthquakes. The most important criteria used to identify Seismites include: 1) the deformation occurs in laterally continuous, recurring horizons, separated by layers of undeformed sediment that can be temporally or stratigraphically constrained; 2) the deformation involves alluvial, lacustrine, and marine sediments; 3) deformed and undeformed beds have similar lithologies and facies features; 4) the deformation can be related to a seismically or tectonically active area when the SSDS were formed; and 5) the deformation shows systematic increases in frequency or intensity toward a likely epicentral area (Seilacher, 1984; Qiao et al., 1994; Obermeier, 1996; Ettensohn et al., 2002; Montenat et al., 2007; Qiao and Li, 2008, 2009; Van Loon, 2009).

Recognition of seismites generally involves a combination of sedimentary facies analysis, identification of potential triggers, and recognition of all of the criteria listed above (Owen et al., 2011). Various SSDS have recently been identified in the Zhucheng faulted depression. The initial recognition of SSDS in the Upper Cretaceous strata was reported briefly after the initial discovery (He et al., 2011). The earlier paper in Chinese reported a large variety of SSDS sedimentary rocks containing the largest collection of dinosaur fossils in Asia (Yang, 1958). So far, approximately 8000 dinosaur fossils, both as individual animals and bone masses, have been recovered from several quarries in the Upper Cretaceous Wangshi Group southwest of Zhucheng (Fig. 1, A, B). In addition, many footprints of different dinosaur species are preserved in sedimentary rocks of the Lower Cretaceous Laiyang Group. Major dinosaur fossils include femurs, humeri, ribs, tibiae and scapulae of hadrosaurs, horned dinosaurs, tyrannosaurus and other species (Yang, 1958; Hu, 1973; Li, 1998; Zhao et al., 2007; Hone et al., 2011). The longest single bone is 4.84 m, the shortest is about 10 cm, and many small skeletal fragments are also present. These fossils were buried in debris flows, or flood plain and braided channel deposits, with the debris flow deposits being the most important (Liu et al., 2003; The Fourth Institute of Geological and Mineral Resources Reconnaissance of Shandong Province, 2003; Liu et al., 2010, 2011). Abundant, well-preserved footprints of dinosaurs are present in the Huanglonggou quarry south of Zhucheng, where ca. 3000 tracks belonging to at least 6 species, including ornithopod, theropod, sauropoda and others, have been identified in an area of 2600 m2, (Li and Zhang, 2000; Li et al., 2001; Xin et al., 2010; Li et al., 2011). Small footprints of ornithopods are generally 5-10 cm long, whereas large footprints of

theropods can be up to 40 cm long (Fig. 1 C, D, E). Most footprints with similar motion orientations are preserved in argillaceous siltstone and fine-grained sandstone of offshore to shallow lacustrine environments with parallel bedding, small-scale cross-bedding and ripple marks (Liu et al., 2011; Li et al., 2011). Why are so many SSDS preserved here and how were they formed? When did they occur? What can they tell us about synsedimentary basin tectonics? Is there any relationship between the occurrences of SSDS and mass burial of dinosaur fossils? In this study we analysed a variety of SSDS in many fossil quarries, including Kugou, Longgujian and Huanglonggou and adjacent areas in the southwestern part of the Zhucheng depression. The sedimentology of the deposits hosting the SSDS is very similar to that of the undeformed beds, which both overlie and underlie the deformed beds. Morphological analysis of the deformational features was used to identify the driving force involved and the mechanism of deformation. Our goal was to use the SSDS and their relationship to facies and architectural elements to reconstruct the tectonic paleogeographic environment existing during deposition of the Yangzhuang Formation and the Wangshi Group. We also carried out U/Pb dating of detrital zircon in the sedimentary rocks containing SSDS in order to place a minimum age on their deposition. Using these data we discuss the variety of SSDS in the different deposition environments and the timing of activity on trigger fault(s). A particular aim was to determine if there was any relationship between paleo-earthquake events and dinosaur fossil burial in this environment. 2. Geological Setting The Zhucheng depression is a triangular-shaped feature located in the southwestern

portion of the Jiaolai Basin, Jiaodong Peninsula, eastern China. It is bounded on the south by the Wulian fault and on the western and northern margins by the Yishu and Baichihe faults, respectively (Fig. 2). The ENE-striking Wulian normal fault extends for 140 km, and has a vertical displacement of 1000-2000 m (Zhang et al., 1997; Zhang et al., 2008; Li et al., 2012). The Yishu fault marks the eastern boundary of the middle Tan-Lu fault zone (Xu, 1984). This fault experienced mostly normal displacement during the Early Cretaceous, despite the complex history of the Tan-Lu system (Yin and Nie, 1993; Li, 1994; Xu and Zhu, 1994). The Baichihe fault is a south-dipping, listric normal fault, 50 km long, that was active during the Cretaceous (Dai et al., 1995; Chen and Dai, 1998). These major faults constrained the development of stratigraphic sequences in the Zhucheng depression, including the Lower Cretaceous Laiyang and Qingshan Groups, and the Upper Cretaceous Wangshi Group (Song et al., 2002; Shi et al., 2003; Zhang et al., 2006; Yin and Yang, 2005; Liu et al., 2010, 2011). The Laiyang Group is composed of 5 formations, which are from the base upward, the Linshansi, Zhifengzhuang, Yangzhuang, Qugezhuang, and Fayin (Fig. 3) (Zhai, 2003; Zhang et al.2003; Song et al., 2002). The fossil-rich Laiyang Group, which is about 2000 m thick, was deposited in a piedmont, pluvial-fluvial-lacustrine environment. The Linshansi Formation is mainly composed of the purplish-grey polymict conglomerate and coarse-pebble, feldspathic sandstone, typical of alluvial fans. The Zhifengzhuang (Shuinan) Formation consists of grey to greyish-brown, pebbly sandstone with interbeds of tuff, siltstone and shale, formed in a fluvial to shallow lacustrine setting. The Yangzhuang Formation is divided into three cycles; each of which consists, from the base upward, of grey sandstone, siltstone and grey-green mudstone and shale. Asymmetrical ripple marks are common in the lower part of the formation, whereas

cross-bedding and inclined bedding are well-developed at the top. The mudstones and shales in this formation are rich in fossils, and contain many SSDS. The Qugezhuang Formation grades upward from light grey and yellowish-green, silty shale to purplish-grey, conglomeratic and coarse-grained sandstone, indicating development of a fluvial environment. Clasts in these sedimentary units consist mostly of volcanic rocks, granite, vein quartz and quartz. Some lava flows are also present in this formation. Along the eastern and southern margins of the Jiaolai Basin, the Lower Cretaceous Qingshan Group, composed mainly of volcanic and volcaniclastic rocks, unconformably overlies the Laiyang Group. The Wangshi Group includes the Lower Cretaceous Linjiazhuang and the Upper Cretaceous Xingezhuang Formations, as well as the Upper Cretaceous Hongtuya Formation, all of which are composed mainly of alluvial fan and floodplain deposits. The Linjiazhuang Formation, which unconformably overlies rocks of the Qingshan Group, consists of greyishpurple, polymict conglomerate intercalated with purple, fine-grained siltstone. In contrast, the Xingezhuang Formation consists mainly of yellowish-green to greenish-grey, fine-grained, sandstone with some intercalated mudstone and conglomerate at the base. The upper part contains many gastropod and bivalve fossils, typical of shallow, lacustrine depositional environments. The Hongtuya Formation is dominated by greyish-purple, polymict conglomerate, gravel, sandstone and siltstone, with some intercalated basalt, indicating deposition in a fluvial environment. The thickness of this formation varies dramatically from about 700 m to 4000 m (Song et al., 2002). Numerous dinosaur skeleton fossils and paleoearthquake records have been identified in sandstones and conglomerates of the upper parts of the Xingezhuang and Hongtuya Formations.

Three phases of Cretaceous volcanic activity are recognized in the study area. A basalt flow in the middle of the Yangzhuang Formation southeast of the Jiaolai Basin has a zircon U/Pb age of 129.4 ± 2.3 Ma (Zhang et al., 2008). Slightly younger U/Pb ages ranging from 120 to 105 Ma have been obtained from volcanic rocks of the Qingshan Group (Qiu et al., 2001), and a basalt flow at Daxingzhuang, northwest of Qingdao, has an

40

Ar-39Ar plateau age of

73.2 ± 0.3 Ma (Yan et al., 2003, 2005). 3. SSDS and their driving forces 3.1 Undulate folds: 3D geometry - ‘egg-box or bowl’ structures Several sedimentary layers with SSDS occur in the Huanglonggou quarry (Fig. 4), where numerous dinosaur tracks have been found. A single, well-defined layer with numerous undulate folds is bracketed by two undeformed layers. Both the deformed and undeformed layers are grey mudstone, silty mudstone, and interbedded light grey siltstone, with thicknesses of about 5-7 cm. Ripples are well-preserved on some of the undeformed layers (Fig. 1C), and undulate folds with an “egg-box” or “bowl” appearance are widespread in the deformed layers. The folds in these layers form wide synclines connected to narrow anticlines with amplitudes of about 17 cm. The anticlines are thickest at the tops of the folds and thinnest at the limbs, and the axial planes generally dip at angles of about 65~85° (Fig. 4A, 4B). The deformed layers show two superimposed folds, one striking WNW with a wavelength of about 35-45 cm, and the other NNW with a wavelength of about 10 cm. Thus, these two folds produce 3-dimensional features similar to open, round bowls, which when arranged together, have an ‘egg box’ appearance (Fig. 4D). This kind of SSDS occurs in unconsolidated sediments which are rich in water. Thin layers of clay and silt interbedded with laminated sand layers are nearly horizontal.

The two generations of folds indicate formation by interfering compressional stress fields in NNW-SSE and nearly E-W directions. The deformed layers are overlain by undeformed layers containing numerous dinosaur footprints, aligned in the same general direction, and with approximately the same motion orientation. 3.2 Convoluted deformation structures and seismic unconformities Convoluted deformation structures are recognized in the Upper Cretaceous Yangzhuang Formation of the Laiyang Group in the northern section of the Huanglonggou quarry (Fig. 2, site 4). The layers containing these features are about 2-5 cm thick and are composed mostly of dark grey, argillaceous silt with thin bands of grey sand (Fig. 5A). These deformed layers display plastic-flow folds, and some small liquefaction veins (Fig. 5B). The veins consist of sand which was liquefied and injected into the overlying layers of mud or silt. The convoluted deformation structures usually accompany seismic unconformities. After deformation, the tops of some convoluted structures were eroded, leading to abrupt contacts with the overlying layers (Fig. 5B, 5D). These zones are identical to those described elsewhere by many authors (Liang et al., 1991, 1994; Moretti et al., 1999; Qiao et al.., 2008; Qiao and Li, 2009; Yang et al., 2008) and are termed seismic unconformities. 3.3 Mound-and-sag structures Mound-and-sag deformation structures (Rossetti et al., 2000) have been recognized in some layers exposed in the northern section of the Zhucheng depression (Fig. 2, spot 4), where deformed layers are intercalated with thick, undeformed layers (Fig. 5C, Fig. 5E). Both the deformed and undeformed layers consist of light grey sandstone and grey silt or silty mudstone.

The sandstone layers are generally 5-10 cm thick, whereas the silt and silty mudstone layers rarely exceed 6 cm. The axial planes of mound-and-sag structures with wide sag and narrow mounds are parallel, but the curvature of the inner arc fold in each mound is larger than that of the outer arc. The mound amplitude is ca. 75 cm. These features were formed by compressional stress. Diapirs can be observed in the cores of some of the mounds (Fig. 5E). These were formed by liquefaction of underlying layers of fine sand, covered by thin horizontal laminae of silt and mud. When liquefied by an earthquake, the fine sand intruded the overlying unconsolidated sediments. Narrow veins of sand commonly occur at the tops of the intrusions, typically pinching out upward and ending in the overlying bed. The intrusion of liquefied sand caused thinning at the tops of the mounds and thickening of their limbs. Depending on the strength of the earthquake activity and the homogeneity of the overlying beds, the sand intrusions penetrated one to several layers in the sedimentary cover. The liquefied sand veins and diapirs exist only at the bottoms of the mounds, so other parts of the mound-and-sag structures have not been affected by liquefaction. 3.4 Liquefied sand veins and liquefied breccias Sand veins are formed by emplacement of liquefied sand flow (Qiao et al., 1994; Obermeier, 1996). Such veins are primarily vertical but some can intrude along bedding planes. Good examples have been observed in the Lower Cretaceous strata at Huanglonggou (Fig. 6).Along with the liquefied sand veins, numerous liquefied breccias developed mainly in sections where thick sandstone layers are interbedded with thinner mudstones. Some of the best examples can be observed on outcrops in the northern quarry, which contain many dinosaur

tracks (Fig. 2, site 5). At that location thin layers, 2-4 cm thick, of greyish-green clayey breccia are sandwiched between thicker layers of light grey sandstone (Fig. 6A, B). The clayey breccias have various shapes, and consist of poorly sorted, angular-subangular fragments, mostly 0.3-3.5 cm in size. The clayey breccias may be separated by liquefied sand veins but in some cases the breccias can be correlated across the veins (Fig. 6A). The unconsolidated mud breccias were formed by intrusion of liquefied sand veins with thixotropic, emplacement and tearing (Qiao et al., 1994, 2006; Du and Han, 2000; Tian and Zhang, 2006; Montenat et al., 2007; He et al., 2010, 2014; Qiao et al., 2012). The formation of these breccias was not associated with slope collapse, fault activity or erosion. 3.5 Plunged sediment mixtures Plunged sediment mixtures (Rossetti et al., 2011) result from mixing of sands derived from two different unconsolidated stratigraphic units, either superposed upon boundaries between the sand bodies of different sources, or present within one another (Fig. 7). A layer containing plunged sediment mixtures occurs above the dinosaur fossil layers at the Kugou quarry. The upper unit involved (Fig. 7C, 7D) consists of brown, pebbly, fine-grained sandstone composed chiefly of lithic fragments (65-70 vol %) which consist of tuff, rhyolite, silica, claystone and andesite. The grains are sub-angular to sub-rounded and poorly sorted, with grain sizes mainly in the range of 0.05-0.5 mm, but with a few up to 10 mm. The grains are cemented by calcite and silica. The lower unit of the deformed layer (Fig. 7E, 7F) consists of greyish-green, pebbly, medium-grained lithic sandstone with the same composition and sedimentary structures as those of the upper unit, except for having a slightly coarser-grained texture. When an earthquake occurred, loose sand of the upper unit interacted with sediment of

the lower unit, which may have been harder or had a higher density than the upper part. The deformation occurred at the boundary between these two units, producing discontinuous undulate surfaces. Fractures were generated at the top of the lower unit, and the sediments of the upper unit sank into the fractures. Spherical, mushroom-shaped and ellipsoidal bodies (Fig. 7A, B) of the lower unit also invaded the upper unit by liquefaction and diapirism. 3.6 Load, ball-and-pillow and injection structures Load structures are laterally persistent and continuous undulations at an interface between two layers of different density, with relatively denser sediments above and less dense sediments below (inverse density gradient). The deformation, size, and triggering of load structures have been discussed and simulated (Kuenen, 1958; Moretti et al., 2002；Moretti and Sabato, 2007; Yan et al., 2007; Qiao and Li, 2008; Qiao and Li, 2009; Owen et al., 2011). Load structures are widely present in sandstone and gravel layers (Fig. 8) of the Upper Cretaceous Hongtuya Formation at the Kugou and Longgujian dinosaur fossil quarry. The layers containing the load structures are intercalated with undeformed layers. The scale of the load structures is variable with heights ranging from 20 to 30 cm, and widths from 60 to 80 cm; the smallest load is at the centimeter scale. Coarse, unconsolidated gravels and sands deposited in braided fluvial channels with horizontal bedding were drawn by gravitational forces, especially during shaking, into the lower unconsolidated fine-grained sediments, which had previously been deposited on a flood plain. The load structures are usually connected with the host layer (native rock) (Fig. 8). Moreover, the load casts may continue to descend to form an isolated body, such as a ball (Fig. 8D, Fig 8E), pillow or bag (Fig. 9B) (so-called ballpillow structures) (Fig. 8D，8E).

Load structures also reflect obvious gravitational effects under shaking. Fine-grained saturated sediments flow downward faster than larger pebbles, forming reverse size grading (Fig. 8A, 8C). Load structures are separated from each other, and do not extend far in a lateral direction. A vertical, pebbly sand dyke is present west of the Longgujian quarry (Fig. 9B). The dyke is a steeply inclined body of sandstone and conglomerate that has sunk downward to form elongated shapes 10 cm long and 5 cm wide that are connected with the overlying host sediments (Rossetti et al. 2011 named this feature a pebbly pocket). The light grey, coarsegrained sediments liquefied downward into the underlying sediments; and the long axes of the pebbles are aligned parallel to the walls of the dyke, indicating liquefied flow. Injection structures are usually accompanied by load structures. The injection part consist of argillaceous sandstone and conglomerate rich in silt. Under abnormal pressure, the underlying sediments are injected upward, but do not penetrate the overlying conglomerate and coarse sand layers. The top of the injection is irregular, showing flexure and branching, sometimes like a flame (called flame structure, Fig. 8B, Fig. 9 A, C). Injection structures can form either as a diapir of liquefied material from the underlying layer or by load cast squeezing. 3.7 Fault grading and syn-sedimentary faults Fault grading and syn-sedimentary faults can be observed occasionally in the Hongtuya Formation at the Kugou and Longgujian dinosaur fossil quarries. Fault grading was first proposed by Seilacher (1969), and is recognized by a liquefied zone, a disorganized rubble zone and a step-faulted zone, with gradational contacts between these zones at the bottom and a sharp boundaries at the top. This pattern reflects strong earthquake shaking of aqueous,

argillaceous sediments in a basin with geopetality, which usually occurs on the paleoslope. Fault grading in the Hongtuya Formation typically involved multiple normal faults dipping northeast at angles of 50°-60°, with offsets of 10-30 cm (Fig. 10A). The faults cut a set of horizontal, flood-plain sediment layers, composed of brownish-gray and light grey silt interbedded with fine-grained to conglomeratic sand. Strata correlated across the faults are thicker in the hanging wall blocks than in the footwall blocks. Pre-existing fault grading was reactivated multiply to form syn-depositional faults, with offsets of 50-110 cm. Collapsed fragments and coarse gravels are located in the hanging wall near the fault plane (Fig. 10B). The fault offsets gradually decrease toward the ENE, and small, collapsed and rotated fault blocks are normally present at the ends of a series of faults (Fig. 10C). A bedding-parallel liquefied vein is present near the fault (D area of Fig. 10A), which formed when the fault was active. Coarse-grained, light grey to yellowish-green aqueous sand layers intruded reddishbrown, fine-grained sediments, as a result of liquefaction along the fault zone. 4. Geochronology of the deformation events 4.1 Analytical methods The SSDS in Shandong Province developed during or shortly after deposition of the sediments and before significant diagenesis. The youngest age of sediment deposition, combined with stratigraphic data should provide an approximate age for the deformation that produced the SSDS. Samples of sandstones and pebbly sandstones with load cast structures were collected from Lower Cretaceous (Sample ZC-32) and Upper Cretaceous (Sample ZC-4) strata. The sample locations are shown in Figures 3 and 14, respectively.

The non-magnetic heavy mineral fraction was separated from these samples using conventional magnetic and density techniques in the Regional Geological Investigation Laboratory of Langfang in Hebei Province. Zircon grains were then hand-picked under a binocular microscope, mounted in epoxy along with zircon standard 91500 and ground to approximately one-half of their thickness. All of the zircons were imaged with transmitted and reflected light as well as cathodoluminescence (CL) in order to determine their shapes and internal structures. LA-MC-ICP-MS zircon U–Pb analyses were performed at the Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing using laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS). The detailed operating conditions for the laser ablation system and the MC-ICP-MS instrument and data reduction were the same as described by Hou et al. (2009). Zircon GJ-1 was used as an external standard for U-Pb isotope fractionation correction (Jackson et al., 2004). U, Th and Pb concentrations were calibrated using zircon M127 (with U:923 ppm; Th:439 ppm; Th/U: 0.475.; Nasdala et al, 2008) or NIST610 (Pearce et al., 1996). Time-drift correction and quantitative calibration for U-Pb dating were performed by ICPMSDataCal (Liu et al., 2010). The data were reduced and presented with the ISOPLOT 3.0 program of Ludwig (2003). The ages used for Fig. 12 and in subsequent discussions are based primarily on 206

207

Pb/206Pb ratios for ages >1 Ga and on

Pb/238U ratios for ages < 1 Ga (Gehrels et al., 1999). Only data with degrees of concordance

less than or equal to 10% were used in the final age calculations (Gehrels et al.; 1999; Nelson and Gehrels, 2007; Naipauer et al., 2010). All analytical data and uncertainties in age are given in Tables 1 and 2. Only data with a 95% confidence level (±2 σ) were used.

4.2 Analytical results In total 191 detrital zircon grains were analyzed from samples ZC-32 and ZC-4. Most of the analysed grains are colorless to slightly pink, euhedral, prismatic or tabular crystals. These crystals have lengths of 40-200 µm and length to width ratios ranging from 4:1 to 2:1. In CL images, most zircons exhibit oscillatory zoning (Fig.11), typical of a magmatic origin, although a few show metamorphic textures. The detrital zircons have a large range of Th and U contents but all have Th/U ratios greater than 0.5 and most ratios are greater than 2. Such values are also characteristic of magmatic zircon. In all cases, we analysed the cores of the zircon grains. Of the 195 analyzed grains, 140 yielded concordant or nearly concordant ages; 53 grains from sample ZC-32 and 87 from sample ZC-4 (Tables.1 and 2). Zircons from the Lower Cretaceous sample ZC-32 yielded eight main age populations (2536, 2198, 897, 691, 444, 296, 123, and 118 Ma), whereas those from the Upper Cretaceous sample ZC-4 yielded seven populations (2477, 1995, 711, 455, 237, 122, and 101 Ma). These zircon age groups are somewhat similar to those of sedimentary rocks of the Zhoucun, Mengyin, and Pingyi Mesozoic Basins, which are located opposite the Zhucheng depression across the Tanlu strike - slip Fault Zone (Yang et al., 2013). They are even more similar to zircon populations in the Laiyang Group in the northern and southern Jiaolai Basin (Xie et al., 2012). Samples ZC-32 and ZC-4 contain relatively few metamorphic zircons of Precambrian age suggesting that they may have been derived from proximal source areas. This interpretation is supported by euhedral to subhedral nature of the zircon grains, which show little abrasion. The age spectra of samples ZC-32 and ZC-4 (Fig.12, 13), show that most valid age lie between 118 to 135 Ma and 101 to 135, respectively.

4.3 Age constraints on the SSDS formation Detrital zircon geochronology has been used extensively over the last few decades to determine the age, lithology and location of clastic sediment sources (Dickinson and Gehrels, 2003; Naipauter et al., 2010; Gehrels, 2012, 2014; Yang et al., 2013). This approach has been particularly useful for determining the provenance, constraining depositional age, quantifying budgets of sediment generation, reconstructing transcontinental dispersal pathways, refining stratigraphic correlations, and characterizing source regions on a local to global scale. In this study, the detrital zircon U-Pb ages are used to identify the youngest depositional age of the sediments containing SSDS in order to place an approximate lower time limit on the formation of the SSDS. As pointed out above, the formation of the SSDS must have occurred very shortly after sediment deposition. . The youngest detrital zircons from sample ZC-32 form a group of 12 grains ranging in age from 118±1 Ma to 125±0 Ma. They represent 23% of the reliable ages with high degrees of concordance (100%) (Table 1) and suggest a lower age limit of approximately 118 Ma. Plant fossils, including Y. sinensis, Y. chekiangensis and Y. kyongsangensis of the Yanjiestheri fauna occurring in rocks of the Laiyang Group in the Zhucheng depression are representative of a conchostracans assemblage with an Early Cretaceous age (Song et al., 2002). Zircon U/Pb ages from volcanic rocks of the Qingshan Group range from 120 to 105 Ma (Qiu et al., 2001), similar to the detrital zircon ages. The stratigraphic sequence from which sample ZC-32 was collected was probably deposited somewhere between approximately 118 Ma and 105 Ma, indicating a similar age for the Early Cretaceous SSD events.

The youngest zircons recovered from the Late Cretaceous sample ZC-4 of a cluster of ages ranging from 101±2 Ma to 116±3 Ma (Table 2). This group of 16 analyses makes up 19% of the reliable ages from this sample and all have a degree of concordance (97%-100%). These dates suggest that the depositional age was no younger 101 Ma. Fossils from the Hongtuya Formation in the Zhucheng depression include Cypridea sp., Eucyprs sp., Talicypridea amoena, E.bullata, Candona sp. and Candoniella sp. Talicypridea is a widely distributed and stable genus of ostracods with a Late Cretaceous age. Also present are Shantungosaurus giganteus and Tyrannosaurus cf.res in the Hongtuya Formation that span the period between Early and Late Cretaceous (Hu and Chen, 1986; Song et al., 2002). Bivalves, such as Pseudohyria cardiiformis, P. aff.gobiensis, Plicatounio zhuchengensis, Sphaeriumtani and S.shantungense, are also common in these rocks and were well developed in the Late Cretaceous (Song et al., 2002) or in the end of the Early Cretaceous - early Late Cretaceous (Sha, 2007). All of the available data place the strata from which sample ZC-4 was collected in the early Late Cretaceous. The Zhucheng basalts, which are included in the Hongtuya Formation crop out located at about 10 km west of the Longgujian dinosaur fossil quarry and these have a whole-rock K-Ar date of 76 Ma (Meng et al., 2006). On the basis of the available stratigraphic and geochronological data, the deformational events that produced the SSDS in the Zhucheng depression took place between approximately 100 Ma and 76 Ma (Meng et al., 2006), with the detrital zircon ages favoring the early part of this range. Obviously, the time span is large, and more data are needed, particularly from the Zhucheng basalts, to obtain a more precise age. However, we suggest that the deformation in the Upper Cretaceous took place shortly after 100 Ma.

5. Discussion of deformation mechanisms and their implications 5.1 Distribution of the SSDS The SSDS in the Zhucheng depression occur in distinct layers in a sedimentary sequence, which are separated by undeformed layers. At least 8 distinct layers containing SSDS are visible in the exposed sequence at the Huanglonggou quarry and at 3 exposed sections in the adjacent area (Fig. 14, spot 3, 4, 5), 4 layers are present in the Kugou quarry (Fig. 14, spot 1) and 5 layers are present in the Longgujian quarry (Fig. 14, spot 2). These layers of SSDS occur in sedimentary sections ranging from 15 to 20 m thick. The SSDS in the Shandong Peninsula have a wide range of morphology and style. Those preserved in the Upper Cretaceous sedimentary rocks are mainly load structures, injection structures, fault-graded beds and liquefied sand veins, whereas undulate folds and convoluted deformation structures are confined to the Lower Cretaceous sections. The Lower Cretaceous Yangzhuang Formation of the Laiyang Group consists mainly of lacustrine sedimentary rocks, including fine sand, silt and mud. Thus, this formation was generally weak and had little competency, and thus was susceptible to convolute deformation and folding. On the other hand, the Upper Cretaceous Xingezhuang and Hongtuya Formations of the Wangshi Group are mainly composed of coarse sand, gravel and conglomerate deposited in alluvial fan and flood-plain settings. These deposits were stronger, with a larger competency, and were thus able to form load structures and plunged sediment mixtures in response to tectonic activity. All these observations indicate that the lithology, lithofacies and sedimentary facies of sediments can significantly affect the styles of SSDS.

5.2 SSDS triggered by seismic activity All of the SSDS in study area occur in alluvial-lacustrine sediment layers, which are laterally continuous and separated vertically by undeformed sediment. Both the deformed and undeformed layers have similar lithologies and facies characteristics. The intensity, complexity and abundance of the SSDS form zonal patterns and they all satisfy the criteria (as described in the Introduction) needed to demonstrate their relationship to seismic activity (Seilacher, 1984; Qiao et al., 1994; Leeder, 1987; Obermeier, 1996; Ettensohn et al., 2002; Montenat et al., 2007; Qiao and Li, 2008, 2009; Owen et al., 2011). Thus, we propose that all of the observed deformation in the area was seismically triggered. Each layer containing SSDS, separated by undeformed layers, is considered to reflect a single seismic event, thus the multiple layers observed in the area suggest frequent seismic activity. 5.3 Analysis of paleo-seismic activity The Zhucheng depression is surrounded by boundary faults; on the west is the NNEtrending Yishu strike-slip fault (the middle part of the Tanlu fault), on the north is the EWtrending normal Baichihe fault and on the south is the ENE-oriented Wulian fault. Is it possible to determine which the seismogenic fault was? The mound-sag structures of the Laiyang Group were formed by unidirectional shortening triggered by simple compression, whereas the undulate folds were formed under multidirectional, interfering compressional stress. On the basis of the rheological behavior of cohesionless sediments and the associated deformational structures, the deformational mechanisms were likely hydro-plasticity, liquefaction and fluidization, which reflect increasing deformational strength (Lowe, 1975; Allen, 1977; Owen, 1987; Guiraud and Plaziat, 1993;

Qiao et al., 2008). The type of SSDS in the Yangzhuang Formation changes upward from plastic convolute deformation to liquefied vein to liquefied breccia (Fig. 14), implying that the seismic activity was stronger in the later period than in the early period. The abundance of paleo-seismic records decreases to the north, suggesting that movement on the Wulian fault was responsible for the early deformation under weak compressional stress. Load structures, fault grading and syn-sedimentary faults, liquefied veins and plunged sediment mixtures are the dominant deformational features in the Upper Cretaceous, and these are all interpreted to have formed in an extensional environment (Qiao et al., 1994; Rossetti et al., 2011). Load structures, fault grading and ball-pillow deformation structures are thought to be triggered by 5-8 Ms intensity earthquakes (Rodriguez-Pascua M.A, 2000; Tian and Zhang, 2006); other features such as plunged sediment mixtures, boudinage, liquefied breccias and mound-sag structures are thought to be triggered by smaller magnitude earthquakes (Ferreira et al., 1998, 2008; Bezerra et al., 2007; Liang et al., 2009; He et al., 2010, 2014; Rossetti et al., 2011). On the basis of the distribution of load structure along the strike of the strata (nearly EW), the Wulian fault is thought to be the most likely seismogenic feature for this deformation, which involved N-S extension during deposition of the Hongtuya Formation. 5.4 Age of SSDS deformation and triggering fault Stratigraphic correlations, the ages of the associated volcanic rocks (Qiu et al., 2001; Yan et al., 2003, 2005; Zhang et al., 2008), and the detrital zircon ages indicate that the Early Cretaceous SSDS in the Zhucheng depression were formed about 118-105 Ma (Fig. 12), whereas the Late Cretaceous features probably formed around 100 Ma or a little later. Previous studies suggested that the SSDS in the Early Cretaceous were formed at about 129-

120 Ma and that the younger features formed somewhere between 105 and 73 Ma on the basis of regional magmatic events (He et al., 2011). This earlier study also suggested that the Wulian fault, along which the paleoseismic activity occurred, operated in a compressional stress field during the period between 118 Ma and 105 Ma but shifted to an extensional stress field from 100 Ma to 76 Ma. 5.5 Relationship between paleo-earthquake events and buried dinosaur fossils Paleo-earthquake records in the middle of the Early Cretaceous Yangzhuang Formation indicate that the seismic activity was periodical, frequent and related to weak compressional stress, corresponding to the assumed regional stress at that time (Zhang et al., 2008). Both the stratigraphic sequences and tectonic activity recorded in the Yangzhuang and Qugezhuang Formations indicate deposition in continental extensional environments, and the environment changed from lacustrine to fluvial, with the lacustrine depocenter moving northwest of Huanglonggou (Ren et al., 2008; Liu et al., 2011). Diverse dinosaur tracks in the Early Cretaceous Laiyang Group (Li et al., 2011) are mainly footprints of theropods and ornithopods that were able to live in lacustrine and swampy environments (Zhao et al., 2007; Li, 2010). Because regional tectonic activity and seismic events changed the local environment, the dinosaurs may have migrated to the swampy areas containing lush vegetation, after the paleo-earthquake events, possibly accounting for the aligned footprints oriented in about the same direction. Dinosaur skeleton fossils in the Upper Cretaceous Wangshi Group were buried in debris flows and flood plain and braided-channel deposits (Liu et al., 2010). The fossils are oriented with a preferred direction of approximately N-S (He et al., 2011), indicating that they

were transported by high energy debris flows in that direction. According to the gravel component of the sediments and the fossil distribution, the paleo-currents were from the SSW to the NNE (Zhang et al., 2008; Liu et al., 2011; He et al., 2011). The conglomerate clasts were derived mainly from rocks of the Laiyang and Qingshan Group, and deposited near their source. Earthquakes usually occur on the margins of tectonic plates, and debris flows and landslides are mostly distributed along rising mountains and seismically active belts. Debris flows produced by earthquakes are periodic and widely distributed (Kastens, 1984; Ma and Shi, 1996). Between the Early to Late Cretaceous, the Sulu orogenic belt in the southern part of the Zhucheng depression was uplifted rapidly (Zhang et al., 1997; Yin and Yang, 2005), leading to strong weathering of the strata and denudation. Large-scale debris flows and alluvial fans occurred in the southern areas between the basin and the orogenic belt. The debris flows and flood-plain sediments buried the dinosaur fossils. The magnitude of paleo-earthquakes in the area generally alternated between large and small, so we suggest that burial of the dinosaur fossils was associated with the high-energy seismic events. Large-scale debris flows induced by paleo-earthquakes transported the dinosaur skeletons and buried them in the present KugouLonggujian area. 6. Conclusions (1) Various brittle and plastic SSDS are preserved in the Cretaceous strata exposed in dinosaur fossil quarries in Zhucheng, Shandong Province. The structures include undulate folds, diapirs, liquefied breccias, liquefied sand veins and plunged sediment mixtures, fault-

graded beds, convolute deformation and seismic unconformities, as well as load-and-injection structures. (2) The sediment properties, competency of the strata, driving force and deformational mechanism combined to determine the morphology and style of the SSDS. In the middle part of the Early Cretaceous Laiyang Group, SSDS are mainly mound-sag features formed under unidirectional compressive stress, whereas the associated undulate folds formed under multidirectional interfering compressional stresses. In the Upper Cretaceous Lower Wangshi Group SSDS are mostly load structures and fault-graded beds formed in an extensional setting. (3) On the basis of their morphology and distribution, the observed SSDS in the Zhucheng depression are identified as seismites. Stratigraphic correlations, associated magmatic events and detrital zircon ages indicate the paleoseismic activity took place both in the Lower Cretaceous between about 118-105 Ma, and in the Upper Cretaceous at around 100 Ma. (4) The distribution of paleo-seismic records and intensity of the paleo-earthquakes suggest that the seismic activity was associated mainly with the Wulian fault. The possible effect of the Tanlu fault needs to be further investigated. We propose that burial of dinosaur tracks may have been induced by earthquake activity and environmental changes resulted in dinosaur migration in the early Cretaceous. Late Cretaceous buried dinosaur skeletons are associated with large-scale debris flows and frequent earthquake events. (5) Study of SSDS can help to establish a relationship between sedimentary setting and tectonic evolution, constrain the location and timing of tectonic events, and provide evidence for changes in sedimentary environments.

Acknowledgements This study was supported by a Special Research Grant from Ministry of Land and Resources of the People’s Republic of China (No. 201011034), the Science Research from SINOPEC (P05036, KY2013-s-024), and the Innovation Group of National Natural Science Foundation of China (No. 40921001, 41272066). We are grateful to academician Zhiqin Xu and Prof. Jingsui Yang for their supporting of this project, and thank Professors Yongqing Liu, A.J.(Tom) Van Loon, Zeming Zhang, Xuexiang Qi, Zengqi Zhang, Fancong Meng, Hongwei Kuang, Lingsen Zeng and Associate Professor Xin Dong for their contributions of helpful data. Professors Haibing Li, Tiannan Yang, Marie-Luce Chevalier, and Tianfu Li contributed many helpful modifications to the manuscript. We are also grateful the Guest Editor, Professor Paul T. Robinson for his insightful and constructive editing and review.

References Allen, J.R.L., 1977. The possible mechanics of convolute lamination in graded sand beds. Journal of the Geological Society, London 134, 19-31. Allen, J.R.L., 1986. Earthquake magnitude-frequency, epicentral distance, and SSD in sedimentary basins. Sedimentary Geology 46, 67-75. Allen, J.R.L., Banks, N.L., 1972. An interpretation and analysis of recumbent-folded deformed cross-bedding. Sedimentology 19, 257-283. Bezerra, F.H.R., Takeya, M.K., Sousa, M.O.L., Do-Nascimento, A.F., 2007. Coseismic reactivation of the Samambaia fault. Tectonophysics 430, 27-39.

Chen, S., Dai, J., 1998. Features of tectonic stress fields in Jiaolai basin. Journal of China University of Petroleum 22(3), 19-25 (in Chinese with English abstract).Chen, Z., Yang, N., Chen X., 1996. The study of the Indosinian tectonic facies in the Yanshan Area, Acta Geoscientica Sinica 18(1), 11-17 (in Chinese with English abstract) Dai, J., Lu, K., Song, Q., Chen, S., 1995. Kinematics characteristic of Jiaolai basin. Journal of China University of Petroleum 19(2), 1-6 (in Chinese with English abstract). Dickinson, W., Gehrels, G.E., 2003. U–Pb ages of detrital zircons from Permian and Jurassic eolian sandstones of the Colorado Plateau, USA: paleogeographic implications. Sedimentary Geology 163, 29–66. Du, Y., Han X., 2000. Seismo-deposition and seismites. Advances in earth science 15(4), 389394 (in Chinese with English abstract). Ettensohn, F.R., Kulp, M.A., Rast, N., 2002. Interpreting ancient marine seismites and apparent epicentral areas for paleo-earthquakes, Middle Ordovician Lexington Limestone, central Kentucky, In: Ettensohn F.R., Rast, N., Brett, C.E., eds. Ancient Seismites: Boulder, Colorado. Geological Society of America Special Paper 359, 177-190. Ferreira, J.M., Bezerra, F.H.R., Sousa, M.O.L., Nascimento, A.F., Sá, J.M., França, G.S., 2008. The role of Precambrian mylonitic belts and present-day stress field in the coseismic reactivation of the Pernambuco lineament, Brazil. Tectonophysics 456, 111-126. Ferreira, J.M., Oliveira, R.T., Takeya, M.K., Assumpcão, M., 1998. Superposition of local and regional stresses in NE Brazil: evidence from focal mechanisms around the Potiguar Basin. Geophysical Journal International 134, 341-355. Galli, P., 2000. New empirical relationships between magnitude and distance for liquefaction.

Tectonophysics 324, 169-187. Gehrels, G., 2014. Detrital Zircon U-Pb Geochronology Applied to Tectonics. Annual Review of Earth Planetary Sciences 42, 127-49. doi:10.1146/annurev-earth- 050212-124012 Gehrels, G. 2012. Detrital zircon U-Pb geochronology: Current methods and new opportunities. In Busby, C and Azor, A (ed.) Tectonics of sedimentary basins: Recent advances. John Wiley & Sons Ltd Publication, 47-62. Gehrels, G., Johnsson, M.J., Howell, D.G., 1999. Detrital zircon geochronology of the Adams Argillite and Nation River Formation, East-Central Alaska, U.S.A. Journal of Sedimentary Research 69, 135-144. Guiraud, M., Plaziat, J., 1993. Seismites in the fluviatile Bima sandstones: identification of paleoseisms and discussion of their magnitudes in a Cretaceous synsedimentary strike-slip basin (Upper Benue, Nigeria). Tectonophysics 225, 493-522. He, B., Qiao X., Tian, H., Chen, S., Zhang, Y., 2011. Palaeoearthquake event and dinosaur fossil burial of the Late Cretaceous in Zhucheng of Shandong Province. Journal of Palaeogeography 13(6), 1671-1505 (in Chinese with English abstract). He, B., Qiao, X., Xu, Z., Jiao, C., Cai, Z., Zhang, Y., Su, D., 2010. The character and significance of paleo-seismic records of the Late Ordovician in Manjiaer Depression and its adjacent area, Tarim Basin, Xinjiang. Acta Geologica Sinica 84(12), 1805-1816 (in Chinese with English abstract). He, B., Qiao, X., Jiao, C., Xu, Z., Cai, Z., Guo, X., Zhang, Y., 2014. Palaeo-earthquake events during the late Early Palaeozoic in the central Tarim Basin (NW China): evidence from deep drilling cores. Geologos 20(2), 105–123.

Hone, D.W.E., Wang, K., Sullivan, C., Zhao, X., Chen, S., Li, D., Ji, S., Ji, Q., Xu, X., 2011. A new, large tyrannosaurine theropod from the Upper Cretaceous of China. Cretaceous Research 32, 495-503. doi:10.1016/j.cretres.2011.03.005. Hou, K.J., Li, Y.H., Tian, Y.Y. 2009. In situ U–Pb zircon dating using laser ablation-multi ion counting-ICP-MS. Mineral Deposit 28(4):481–492 (in Chinese with English abstract). Hu, C., 1973. The giant hadrosaurid fossil in Zhucheng, Shandong. Acta Geologica Sinica 2,179206 (in Chinese). Hu, C., Chen, Z., 1986. Supplementary notes on research and its development of Shantungosaurue Gianteus. Bulletin of Chinese Academic Geological Sciences 14, 163-170 (in Chinese) Jackson, S.E., Pearson, N.J., Griffin, W.L., Belousova, E.A., 2004. The application of laser ablation-inductively coupled plasma-mass spectrometry to in situ U–Pb zircon geochronology. Chemical Geology 211(1–2):47-69. Kuenen, P.1958. Experiments in Geology, Trans. Geol. Soc. Glasgow 23, 1-28. Kastens, K. A., 1984. Earthquakes as a triggering mechanism for debris flows and turbidites on the Calabrian Ridge. Marine Geology 55(1-2), 13-33 Leeder, M.R., 1987. Sediment deformation structures and the paleotectonic analysis of sedimentary basins, with a case-study from the Carboniferous of northern England. In: Jones, M.E., Preston, R.M.F. (Eds.), Deformation of Sediments and Sedimentary Rocks: Geological Society, London, Special Publication, 29, pp. 137-146. Li, R., Lockley, M.G., Matsukawa, M., Wang, K., Liu, M., 2011. An unusual theropod track assemblage from the Cretaceous of the Zhucheng area, Shandong Province, China.

Cretaceous Research 32(4), 422-432. doi:10.1016/j.cretres. 2010.10.006. Li, R., Zhang, G., 2001. A Preliminary study of nonmarine trace fossils from the Laiyang Group (Early Cretaceous), Laiyang basin, east China. Acta Palaeontologica Sinica 40(2), 252-261 (in Chinese with English abstract). Li, R., Zhang, G., 2000. New dinosaur Ichnotaxon from the early Cretaceous Laiyang Group, in the Laiyang Basin, Shandong Province. Geological Review 46, 605-610 (in Chinese with English abstract). Li, S., 1998. Division and correlation of Jurassic and Cretaceous strata, Shandong. Journal of China University of Petroleum 22(1), 1-4 (in Chinese with English abstract). Li, S., Zhao, G., Dai, L., Liu, X., Zhou, L., Santosh, M., Suo, Y., 2012. Mesozoic basins in eastern China and their bearing on the deconstruction of the North China Craton. Journal of Asian Earth Sciences 47, 64–79. Li, Z., 2010. Visit dinosaur fossil quarry in Zhucheng, Shandong. Fossil 1, 2-8 (in Chinese). Li, Z., 1994. Collision between the north and south China blocks: a crust-detachment model for suturing in the region east of the Tan-Lu fault. Geology 22, 739-742. Liang, D., Nie, Z., Song, Z., Zhao, C., Chen, K., Gong, H., 2009. Seismic-tsunami sequencr and its geological features of Mesoproterozoic Wumishan Formation in Fangshan Global Geopark, Beijing, China: a case study on Yesanpo scenic district. Geological Bulletin of China 28(1), 30-37 (in Chinese with English abstract). Liang, D., Nie, Z., Song, Z., 1994. A re-study on seismite and seismic-unconformity: Taking Western Sichuan and Western Yunnan as an Example. Earth Science-Journal of China University of Geosciences 19(6), 845-850 (in Chinese with English abstract).

Liang, D., Nie, Z., Wan X., Chen G., 1991. On the seismite and seismodisconformity- take the W. Hunan and W. Yunnan regions as an example 5 (2), 138-147(in Chinese with English abstract). Liu, M., Zhang, Q., Song, W., 2003. Division of the Cretaceous lithostratigraphic and volcanic sequences of Shandong. Journal of Stratigraphy 27(3), 247-253 (in Chinese with English abstract). Liu, Y., Gao, S., Hu, Z., Gao, C., Zong, K., Wang, D. 2009. Continental and oceanic crust recycling-induced melt-peridotite interactions in the Trans-North China Orogen: U-Pb dating, Hf isotopes and trace elements in zircons from mantle xenoliths. Journal of Petrology 51, 537-571. Liu, Y., Kuang, H., Peng, N., Ji S., Wang X., Chen, S., Zhang, Y., Xu, H., 2010. Sedimentary Facies and Taphonomy of Late Cretaceous Deaths of Dinosaur, Zhucheng, Eastern Shandong. Geological Review 56(4), 457-468 (in Chinese with English abstract). Liu, Y., Kuang, H., Peng, N., Xu, H., Liu. Y., 2011. Sedimentary facies of dinosaur trackways and bonebeds in the Cretaceous Jiaolai Basin, eastern Shandong, China, and their paleogeographical implications. Earth Science Frontiers 18(4), 9-24 (in Chinese with English abstract. Lowe, D.R., 1975. Water escape structures in coarse-grained sediments. Sedimentology 22, 157204. Ludwig, K.R., 2003. User’s manual for Isoplot 3.0: Geochronological toolkit for Microsoft Excel. Berkeley Geochronology Center Special Publication 4,1-70. Ma, D., Shi, Y., 1996. An approach on effects of earthquakes on formation of debris flow.

Northwestern Seismological Journal 18(4), 38-42. Meng, F.C., Li, T.F., Xue, H.M., Liu, F.L., Xu, Z.Q., 2006. Two serials of basic magmas from different sources ofLate Cretaceous in east Shangdong province, China: A comparative study on basalts from Zhucheng and Jiaozhou. Acta Petrologica Sinica, 22(6):1644-1656. Montenat, C., Barrier, P, dÉstevou, P.O., Hibsch, C., 2007. Seismites: an attempt at critical analysis and classification. Sedimentary Geology 196, 5-30. Moretti, M., Alfaro, P., Caselles, O., Canas, J.A., 1999. Modelling seismites with a digital shaking table. Tectonophysics 304, 369-383. Moretti, M., Pieri, P., Tropeano, M., 2002. Late Pleistocene SSD structures interpreted as seismites in paralic deposits in the city of Bari (Apulian foreland southern Italy) In: Ettensohn F.R., Rast, N., Brett, C.E., eds. Ancient Seismites: Boulder, Colorado. Geological Society of America Special Paper 359, 75-85. Moretti, M., Sabato, L., 2007. Recognition of trigger mechanisms for SSD in the Pleistocene lacustrine deposits of the Sant-Arcangelo Basin (Southern Italy): Seismic shock vs. overloading. Sedimentary Geology 196, 31-45. Naipauter, M., Vujovich, G.I., Cingolani, C.A., McClelland, W.C., 2010. Detrital zircon analysis from the Neoproterozoic-Cambrian sedimentary cover (Cuyania terrane), Sierra de Pie de Palo, Argentina: Evidence of a rift and passive margin system? Journal of South American Earth Sciences 29: 306-326. Nasdala, L., Hofmeister, W., Norberg, N., Mattinson, J.M., Corfu, F., Dörr, W., Kamo, S.L., Kennedy, A.K., Kronz, A., Reiners, P.W., Frei, D., Kosler, J., Wan, Y.S., Göze, J, Höer, T, Kröer, A., Valley, J.W., 2008. Zircon M257 - a Homogeneous Natural Reference Material

for the Ion Microprobe U-Pb Analysis of Zircon. Geostandards and Geoanalytical Research 32(3): 247-265. Nelson, J., Gehrels, G., 2007. Detrital zircon geochronology and provenance of the southeastern Yukon-Tanana terran. Canadian Journal of Earth Sciences 44, 297-316. Obermeier, S.F., 1996. Use of liquefaction-induced features for paleoseismic analysis- an overview of how seismic liquefaction features can be distinguished from other features and how their regional distribution and properties of source sediment can be used to infer the location and strength of Holocene paleo-earthquakes. Engineering Geology 44, 1-76 Owen, G., 1987. Deformation Processes in Unconsolidated Sands. In: Jones, M.E., Preston, R.F. (Eds.), Deformation of Sediments and Sedimentary Rocks: Geological Society of London Special Publication 29, 11-24. Owen, G., Moretti, M., Alfaro P., 2011. Recognizing triggers for soft-sediment deformation: current understanding and future directions. Sedimentary Geology 235, 133-140. Owen, G., Moretti, M., 2011. Identifying triggers for liquefaction-induced soft-sediment deformation in sands. Sedimentary Geology 235, 141-147. Pearce, N.J.G., Perkins, W.T., Westgate, J.A., Gorton, Jackson, M. P., S. E., Neal, C.R., Chenery, S.P., 1996. A compilation of new and published major and trace element data for NIST SRM 610 and NIST SRM 612 glass reference materials. Geostandards Newsletter 21, 115-144. Qiao, X., Guo, X., Li, H., Gou, Z., Su, D., Tang, Z., Zhang, W., Yang, G., 2012. Soft-sediment deformations in the Late Triassic and the Indosinian Tectonic Movements in Longmenshan Acta geological Sinica 86(1), 132-156 (in Chinese with English abstract).

Qiao, X., Li, H., 2008. Pillow, Ball and pillow structures: Paleo seismic records within strata Geological Review 54(6), 721- 730 (in Chinese with English abstract). Qiao, X., Li, H., 2009. Effect of earthquake and ancient earthquake on sediments. Journal of Palaeogeography 11(6), 593- 610 (in Chinese with English abstract). Qiao, X., Li, H., Wang, S., Guo, X., Si, J., Zong, W., 2008 Paleoseismic Evidence of the TalasFerghana Strike-Slip Fault during Early Jurassic, Xinjiang. Acta Geologica Sinica 82(6), 721-730 (in Chinese with English abstract). Qiao, X., Song, T., Gao, L., Li, H., Peng, Y., Zhang, C., Zhang, Y., 2006. Seismic records in strata (Ancient Earthquake). Beijing, Geological Publishing House, pp. 1-263 (in Chinese with English abstract). Qiao, X., Song, T., Gao, L., Peng, Y., Li, H., Gao, M., Song, B., Zhang, Q., 1994. Seismic sequence in carbonate rocks by vibrational liquefaction. Acta Geologica Sinica, 7(3), 243265 (English edition). Qiu, J., Wang, D., Lo, Q., Liu, H., 2001.

40

Ar-

39

Ar dating for volcanic rocks of Qingshan

formation in Jiaolai basin, eastern Shandong province: a case study of the Fenlingshan volcanic apparatus in Wulian County. Geological Journal of China Universities 7 (3), 351355 (in Chinese with English abstract). Ren, F., Liu, Z., Qiu, L., Han, L., Zhang, Y., Cao, Z., 2008. The prototype character of Jiaolai Basin in Cretaceous Laiyang Period. Acta Sedimentologica Sinica 26(2), 221-233 (in Chinese with English abstract). Rodrìguez-Pascua, M.A., Calvo, J.P., De Vicente, G., Gòmez Gras, D., 2000. Seismites in lacustrine sediments of the Prebetic Zone, SE Spain, and their use as indicators of

earthquake magnitudes during the Late Miocene. Sedimentary Geology 196, 81-98. Rossetti, D.F., Bezerra, F.H.R., Góes Ana, M., Neves, B.B.B. 2011. Sediment deformation in Miocene and post-Miocene strata, Northeastern Brazil: Evidence for paleoseismicity in a passive margin. Sedimentary Geology 235(3-4), 172-187. Rossetti, D.F., Goes, A.M., 2000. Deciphering the sedimentological imprint of paleoseismic events: an example from the Aptian Codo Formation, northern Brazil. Sedimentary Geology 135, 137-156. Santos, M.G.M., Almeida, R.P., Mountney, N.P., Fragoso-Cesar, A. R.S., 2012. Seismites as a tool in the palaeoenvironmental reconstruction of fluvial deposits: The Cambrian Guarda Velha Formation, southern Brazil. Sedimentary Geology 277-278, 52-60. Seilacher, A., 1969. Fault-grade beds interpreted as seismites. Sedimentology 13, 155-159. Seilacher, A., 1984. Sedimentary structures tentatively attributed to seismic events. Marine Geology 55, 1-12. Sha, J., 2007. Cretaceous trigonioidid (non-marine Bivalvia)assemblages and biostrati-graphy in Asia with special remarks on the classification of Trigonioidacea. Journal of Asian Earth Sciences 29, 62–83. Shi, W., Zhang, Y., Dong, S., Wu, L., Du, L., 2003. Tectonic deformation and formation and evolution of the Jiao-Lai basin, Shandong: A case study of a deformation analysis of theWangshi and Dasheng Groups. Geological Bulletin of China 22(5), 325-334 (in Chinese). Song, M., Li, Y., Zhan, J., Liang, B., 2002. Regional geological investigation report of Rizhao (1:250000), Shandong. Shandong Geological Investigation Institute 1-600 (in Chinese).

The Fourth Institute of Geological and Mineral Resources Reconnaissance of Shandong Province. 2003. Regional geology of Shandong province. Shandong Map Publishing House, Jinan, pp, 1-970 (in Chinese). Tian, H., Zhang, Z., 2006. Seismite succession of the Paleogene alluvium along the TanchengLujiang Fault Zone in Anhui area, Shandong. Chinese Journal of Geology 41(2), 208-216 (in Chinese with English abstract). Van Loon, A.J., 2009. Soft-sediment deformation structures in siliciclastic sediments: an overview. Geologos 15, 3-55. Xie, S., Wu, Y., Zhang, Z., Qin, Y., Liu, X., Wang, H., Qin, Z., Liu, Q., Yang, S., 2012. U–Pb ages and trace elements of detrital zircons from early cretaceous sedimentary rocks in the Jiaolai Basin, north margin of the Sulu UHP terrane: provenances and tectonic implications. Lithos 154, 346–360. Xing, L., Jerald, D.H., Wang, K., Li, R., 2010. An Early Cretaceous non-avian dinosaur and bird footprint assemblage from the Laiyang Group in the Zhucheng basin. Geological bulletin 29(8), 1105-1112. Xu, Z., 1984. General of the Tancheng-Lujiang rift system. Structural Geology Review. Geological Publishing House, Beijing (3), 39- 46 (in Chinese with English abstract). Xu, J., Zhu, G., 1994. Tectonic models of the Tan-Lu fault zone, eastern China. International Geological Review 36, 771-784. Yan, J., Chen, J., Xie, Z., Zhou, T., 2003. Mantle xenoliths from Late Cretaceous basalt in eastern Shandong Province: New Constrain on the timing of lithospheric thinning in eastern China. Chinese Science Bulletin 48(14), 1570-1574 (in Chinese).

Yan, J., Chen, J., Xie, Z., Gao, T., Foland, K.A., Zhang, X., Liu. M., 2005. Studies on petrology and geochemistry of the Later Cretaceous basalts and mantle-derived xenoliths from eastern Shandong. Acta Petrologica Sinica 21(1), 99-112 (in Chinese with English abstract). Yan, J., Chen, S., Jiang, Z., Zhang, G., 2007. Simulating experiment on genesis of seismoturbidites in rift lacustrine basin. Journal of Palaeogeography 9(3), 277-282 (in Chinese with English abstract). Yang, D., Xu, W., Xu, Y., Pei, F., Wang, F., 2013. Provenance of sediments from Mesozoic basins in western Shandong: Implications for the evolution of the eastern North China Block. Journal of Asian Earth Sciences 76, 12–29. Yang, J., Nie, L., Zhang, L., Yang, J., Zhang, Y., 2008. Reservoir characters and paleoseismic records in Neogene Wunan Oilfield, southwestern margin of the Qaidam Basin. Acta Geological Sinica 86(6), 805-812 (in Chinese with English abstract). Yin, X., Yang, T., 2005. Seismites in the Laiyang Group in the Jiaozhou-Laiyang basin, Shandong province, and their tectonic implications. Geological Review 51(5), 502-506 (in Chinese with English abstract). Yin, A., Nie, S., 1993. An indentation model for the North and South China collision and the development of the Tan-Lu and Honam fault systems, East Asia. Tectonics 12, 801-813. Young, C., 1958. Dinosaur Fossil of Laiyang, Shandong. Palaeont Sin., Ser C 16. Science Publishing House, Beijing, pp, 1- 138 (in Chinese). Zhai, S., 2003. Structural characteristics and evolution in the Laiyang depression of the Jiaolai basin. Petroleum Geology & Experiment 25(2), 137-142 (in Chinese with English abstract).

Zhang, J., Yang, T., Xu, Z., Lv, J., 1997. Extension of Jiaonan Area in Shandong. Acta Geoscientia Sinica 18 (2), 122-128 (in Chinese with English abstract). Zhang, Y., Dong, S., Shi, W., 2003. Cretaceous deformation history of the middle Tan-Lu fault zone in Shandong Province, eastern China. Tectonophysics 363 (3- 4), 243-258. Zhang, Y., Li, J., Liu, Z., Ren, F., Yuan, J., 2006. Detachment systems in deep of Jiaolai basin and their regional tectonic significance. Oil & Gas Geology 27(4), 504-511 (in Chinese with English abstract). Zhang, Y., Li, J., Zhang, T., Dong, S., Yuan, J., 2008. Cretaceous to Paleocene tectonosedimentary evolution of the Jiaolai basin and in the contiguous areas of Shandong peninsular (North China) and geodynamic implications. Acta Geologica Sinica 82(9), 1229-1257 (in Chinese with English abstract). Zhao, X., Li, D., Han, G., Zhao, H., Liu, F., Li, L., Fang, X., 2007. Zhuchengosaurus maximus from Shandong Province. Acta Geoscientica Sinica, 28(2), 111-122 (in Chinese with English abstract).

Figure captions

Fig.1. Dinosaur fossils and footprints in Cretaceous strata of the Kugou and Huanglonggou quarries, Zhucheng depression, Shandong Province, China. A) Bone bed in the middle part of Kugou quarry (view is about 1/8 the length of the whole quarry); B) Detailed view of fossils in the bone bed (hammer is 23 cm long, camera pointing south); C) View of a dinosaur track in the Lower Cretaceous Yangzhuang Formation of the Laiyang Group (letters indicate the locations of the next two photographs; D) Dinosaur footprint in ripple

marked sandstone; and E) Close-up of the dinosaur track (scale is 10 cm long). Photographs A and C are courtesy of the Zhucheng Dinosaur National Geopark.

Fig. 2. Geologic map of the Zhucheng depression A) Location of the Jiaolai basin, Shandong Province, China, B) Sketch geological map of the Jiaolai basin (modified from Zhang et al., 2008); ZCD: Zhucheng depression; GMD: Gaomi depression; LYD: Laiyang depression; CGU: Chaigou uplift. F1: ChangyiDadian fault; F2: Anqiu-Juxian fault; F3: Tangwu-Gegou fault; F4: Yishui-Tangtou fault; F5: Wulian fault; F6: Baichihe fault; F7: Jiaoxian fault; F8: Pingdu fault; F9: Wulonghe fault; F10: Maozhichang fault; F11: East Doushan fault; F12: Guocheng fault; F13: Zhuwu fault; F14: Haiyang fault; F15: Qingdao fault. Black round spots mark sites observed in this study. Spot: 1-Kugou dinosaur skeleton fossil quarry, 2- Longgujian dinosaur skeleton fossil quarry, 3- Huanglonggou dinosaur track quarry, 4- East of Huanglonggou dinosaur track quarry, 5-Northeast of Huanglonggou dinosaur track quarry Fig. 3. Simplified stratigraphic chart and observed paleo-seismic records in Cretaceous strata, Zhucheng（①Song et al., 2002；②Zhang et al., 2008；③Liu et al., 2010; ④Qiu et al., 2001 ；⑤Hu and Chen, 1986; ⑥Yan et al., 2005） Fig. 4. Undulate folds in the Lower Cretaceous Yangzhuang Formation of the Laiyang Group, Huanghua, Zhucheng. A) Undulate folds, at the Huanglonggou excavation site (view towards the north); B) Sketch of undulate fold deformation, showing that the anticline axial planes strike 10°NE and 310°NW, and dip about 67° and 85°, respectively. Note that

the underlying and overlying layers consist of undeformed light greyish-green sandstone and grey mudstone; C, D). Cross-section and planar characteristics of undulate folds, yielding an 'egg-box' (or bowl-like) appearance. The synclines are connected with antiformal folds within interbedded siltstone and mudstone. Fig. 5. Convolute deformation and seismic unconformity in the Lower Cretaceous Yangzhuang Formation of the Laiyang Group. A) Convoluted deformation and seismic unconformity; B) Close up of A) showing laminated sand and mud with hydroplastic folds formed during fluidization, which were then covered by undeformed sediments; C) Multiple deformed layers interbedded with undeformed layers; convoluted deformation, moundsag deformation and liquefied breccias occur in the deformed layers; D) Sketch of convoluted deformation and seismic unconformity. Hydroplastic fold shows recumbent folding (overturned), and partially liquefied sand vein; E) Diapir, ① plastic intrusion (diapir) of liquefied sediment in fine-grained, dark, silty marls; ② upper beds are thinned by intrusion of sand dykes; ③ thickened fold limbs; ④ on-lap deposition after formation of the mound and diapir. Fig. 6. Liquefied sand vein and breccias in the Lower Cretaceous Yangzhuang Formation of the Laiyang Group. A, B) Liquefied breccia and vertical liquefied sand vein, 880 m northeast of the Huanglonggou dinosaur track quarry (view toward the east); C) Vertical liquefied sand vein and fault-graded beds, showing the vein invading layered mud. Small, graded faults with offsets of about 0.5-3 cm cut laminations of sand and mud; ① liquefied breccia; ②liquefied sand vein; ③ fault-graded beds. Fig 7. Plunged sediment mixtures in the Upper Cretaceous Wangshi Group, Kugou, Zhucheng.

A, B) Plunged sediment mixtures, showing that the SSDS occur at the boundary between two layers, and that the underlying sediment was displaced upward due to liquefaction, and the overlying sediment sank down due to shaking and gravity, producing a broad load structure and a large diapir; C, D) and E, F) Photomicrographs of brown, pebbly, finegrained, lithic sandstone of the upper unit and greyish-green, pebbly, medium-grained, lithic sandstone of the lower unit, respectively (each in plane polarized light and with crossed polars). ①unconsolidated or semi-consolidated, coarse, pebbly sand, ② unconsolidated pebbly sand. Fig. 8. Load, ball and pillow structures in the Upper Cretaceous Hongtuya Formation of the Wangshi Group, Kugou-Longgujian quarry, Zhucheng. A) Load structure in the eastern part of the Kugou quarry (view towards the north); B) Load structure (ball-pillow) and flame-like deformation structure west of the Kugou quarry (view towards the north); C) Configuration of pebbly load structures – note that the grain size has changed from fine to coarse; D) load and ball-pillow structures in the central part of Longgujian section (view towards the north) (the person is 180 cm tall); E) Close up of the load structure in D (view toward the north-west; marker pen is 14 cm long) ① load structure, ② injection structure (flame-up), ③ ball or pillow structure. Fig.9. Load structure and liquefied pebbly sand dyke in the Upper Cretaceous Hongtuya Formation of the Wangshi Group, Longgujian, Zhucheng. A) Overall view of western Longgujian, looking towards the north; B) Liquefied sand and gravel dyke, showing that the light-grey sediment became liquefied and was injected downward into the underlying light-brown sediment layers. Note the arrangement of the gravel clasts, whose long axes are

parallel to the edge of the column; C) Load and injection structures showing that dark sand and gravel sank downward through brown sand and that the underlying sediments were extruded upward ① liquefied pebbly sand dyke, ② load, ③ injection. Fig.10. Fault-graded beds and syn-sedimentary faults in the Upper Cretaceous Hongtuya Formation of the Wangshi Group, Longgujian dinosaur fossil quarry. A) Fault grading and syn-sedimentary fault in brown, bedded, pebbly siltstone, east of Longgujian, ①, ② are syn-sedimentary faults with large offset resulting from repeated fault movement. Arrows show a series of normal fault grading features (view toward the south); B) Fault grading with syn-depositional deformation of coarse sediments on the downthrown side of the fault; C) Breakoff and rotation of a fault block, showing laminar bedding at the tail end of the fault. D) Zone in A) illustrates lateral liquefied zone formed shortly after faulting. Fig.11. Cathodoluminescence images of selected detrital zircons in samples ZC-4 and ZC-32 from rocks with load cast structures in the Cretaceous Wangshi Group and Yangzhuang Formation, respectively, showing the dated spots and ages in Ma. Fig.12 Concordia, histogram, and probability plots of ages (Table 1) of detrital zircons in sample ZC-32 from the Zhucheng depression; peak indicate constituent age populations of Table 1. Fig.13 Concordia, histogram, and probability plots of ages (Table 2) of detrital zircons in sample ZC-4 from the Zhucheng depression; peaks indicate separable age populations of Table 2.

Fig.14. Paleo-earthquake records and their distribution in the Cretaceous strata of Zhucheng (observed sites shows in Fig. 2B).

Figure 1

B

(A)

(B)

(D)

D

E

(C)

(E)

Figure 2

120°E

Laizhou Gulf

121°E

Laizhou

Beijing K2w

Jinan

F11

F10 LYD F13

F9 0 500km

A

F8

K1l

K1l

F12 F14

K2w

Weifang g GMD

K1l JC1 K1ds

K2w

K1l

K1ds CGU

F3

K1l

F4

Qingdao

F6 ZCD 36°N

F2

2 1

F5 F1 Wulian K1l

30km

Zhucheng Place name

F15

K2w ZC1

Zhucheng

0

K1q

JC1 Well

F7 Yellow sea

5 3 4

Research area

Fault

Volcanic rocks of K1

K2w

K1q

K1ds

K1l

Wangshi Gr.

Qingshan Gr.

Dasheng Gr.

Laiyang Gr.

Granite of K1 B

Figure 3

Chrono- Rock strati- Thickness stratigraphic graphic unit m unit PleistoQhh hh >5 cene

Lithology

Sedimentary facies

Assemblage biozone Observed squence of Isotopic age paleo-earthquake records

Delta facies 73.2± 0.3 Ma, 40 Ar- 39Ar, ⑥

K 2h

Alluvial fanMeandering river

>377

Paleoseismic event in Longgujian （3times) Ⅰ （Fig 8C-E） ⅠⅢ（Fig 9A-C） Ⅱ （Fig 10A-C）

Hadrosauridae 　　　　⑤

>238 Wangshi Gr.

Upper Cretaceous

>100

Pseudohyria 　　　　① Shallow lacustrine

Paleoseismic event in Kugou

Sphaerium 　　　　①

273 K1-2x

（4 times） ⅠⅢ （Fig 8B） Ⅱ Sample Ⅰ ZC-4 Ⅸ （Fig 7A,D）

Coastal lacustrine

（Fig 1 A- C）

679

K1fg

Qingshan Gr.

Lower Cretaceous

K 1l

Alluvial diluvial fan 108.2 ± 0.6 Ma, 40Ar-39Ar, ④

30~90

K 1s

70~ 330

K 1b

134

K 1h

60-90

Psittacosaurus sinensis, 　③ Volcanic phase 120~115 Ma, ②

40Ar-39Ar,

0 ~ 549

Meandering lacustrine delta

Lycoptera ①

K 1f K 1q

290 ~ 390

K 1y

535 ~ 2000

Shallow lacustrine

Laiyang Gr.

Fluvial facies

129. 4 ± 2. 3 Ma, SHRIMP U-Pb, 　　　　　　②

Shallow lacustrine

330 ~ 400

Deep- semi deep lacustrine

K1ls

>127

Fluvial facies

Pt1zg

<50

Pt1zj

<100

Slate Granulite marble

Fenzishan Gr.

K1z

Lower Proterozoic

Yanjiestheri ① Coastal lacustrine

Paleoseismic event at northeast of Huanghua （6times） （Fig 6） Ⅳ ⅣⅢ （Fig 6） ⅩⅣ （Fig 5C） ⅥⅦ （Fig 5B） Ⅵ Ⅷ （Fig 5 E） Paleoseismic event in Huanghua （2times） （Fig 1 F- H）

Nakamuranaia 　　　　　①

Load structure Ⅰ

Graded fault Ⅱ

Liquified sand vein Ⅲ

Liquified breccia Ⅳ

Undulate fold Ⅴ

Diapir Ⅷ

Plunged sediment mixtures Ⅸ

Dome-trough Ⅹ

Dinosaur skeleton fossil

Dinosaur track fossil

Hydroplastic convolute Ⅵ

ⅤⅠ　　 （Fig 4） Sample Ⅰ　 ZC-32

Seimic unconformity Ⅶ

Figure 4

C

A Upper undeformed layers Upper undeformed layers Deformed layers

A

nt ifo rm al fo ld

Synformal fold

310°∠80° 310° 80°

Antiformal fold Axial line 10°∠67° 10° 67° Synformal fold

Deformed layers

Lower undeformed layer Axial line

B

D

Figure 5

Upp er un defo rmed laye rs

Seimic

Uppe r und eform ed lay ers

Lowe r und eform ed lay ers

Liquef ied con volutio n defo rmatio n

B Convolution deformation

Unde form ed

uncon formit y

Lower u ndeform ed layers A Seimic

layer s

uncon formit y

B

Upp er u ndef or m ed la yers

Defo rmed layer s③ Und efor med laye rs Defo rmed laye rs②

Unde form ed

layer s C

Undeform ed layers

Liquefied convolution deformation D

Undeform ed layers

Diapir

Deformed layers

②

④ ①

③

E

Figure 6

0

10cm

① ②

②

② A

②

①

②

①

①

① ② ①

0

5cm

B

Undeformed layers

② ② ② ③

0

10cm

Undeformed layers

C

Figure 7

②

② ①

① ②

0

40cm

A

C

500μm

500μm

E

500μm

500μm

C

0

40cm

D

500μm

F

500μm

B

500μm

D

500μm

Figure 8

Undeformed Layer

①

① ①

② Load structure

① C

Undeformed 0

Layer

20cm A

B

Undeformed Layer

Native rock Native rock

>20mm

~20mm ~15mm Load ~10mm ~8mm <5mm mean grain size

Load structure C

② ① ②

0 20cm

①

① E

③

②

①

D

0

20cm

E

Figure 9

C B

A

③ ② ③

③ ①

②

B

C

Figure 10

SWW

① ②

D

B C

0

1m A

B SWW

F2’ F2 F1

S0

F1’

C

Figure 11

（a）ZC-4-51 ZC-4-51

（b）ZC-4-98 ZC-4-98

（ｃ）ZC-4-103 （ｃ） ZC-4-103

（m）ZC-32-82 ZC-32-82

（n）ZC-32-58 ZC-32-58

（q）ZC-32-80 ZC-32-80

120 101

（d）ZC-4-28 ZC-4-28

123

110

（e）ZC-4-8, ZC-4-8, 9

118

（f）ZC-4-65 ZC-4-65

（p）ZC-32-5 ZC-32-5

122

（o）ZC-32-100 C-32

（r）ZC-32-26 ZC-32-26

122 123

127

123

（g）ZC-4-105 Z

（h）ZC-4-95 ZC-4-95

279

（j）ZC-4-63 C

（k）ZC-4-104 C-4

(A)

（s）ZC-32-2 ZC-32-2 762

237

2456

（i）ZC-4-64 ZC-4-64

124

124

124

（t）ZC-32-18 ZC-32-18

（u）ZC-32-42 ZC-32-42

296 133

442

（l）ZC-4-68 ZC-4-68

（v）ZC-32-27 C

711

1992

100μm

2563

(B)

（w）ZC-32-22 ZC-32-22

（x）ZC-32-99 ）ZC-32-99

900

778

100μm

Figure 12 50

(a)

Number

206

1400 0.2

4 3 2 1 0 115

20 15

1000

120

125

130

135

140

145

10

600 0.1 0.0 0

30 25

9 8 7 6 5

Relative probability

35

1800

0.3

(c)

40

2200

0.4

( c )10

(b)

Relative probability

2600

0.5

Pb/ 238U

45

Number

0.6

5 2

4

6

8 207

235

Pb / U

10

12

14

0 0

400

800

1200 1600 Age(Ma)

2000

2400

2800

Figure 13 100

(a)

Number

Pb/ 238U 206

1400 1000

60 50

8 6 4

40

2

30

0 95

20

600

0.0 0

10

105

115 125 Age(Ma)

135

145

Relative probability

0.3

0.1

12

70

1800

0.2

14

80

2200

0.4

(c)

Relative probability

2600

0.5

( c )18 16

(b)

90

Number

0.6

10 2

4

6 8 235 Pb / U

207

10

12

0 0

400

800

1200 1600 Age(Ma)

2000

2400

2800

Figure 14 (color)

Kugou Spot 1 (K2 h)

East Longgujian Spot 2-1 (K2 h)

North Longgujian Spot 2-2 (K2 h)

8

8

8

7

7

7

6

6

6

5

5

4

4

4

3

3

3

2

2

2

1

1

1

Sample ZC-4

5

0 (m) cl

si

fss mss css peb cob &gran

0 (m) cl

Huanglonggou Spot 3 (K1 y)

si

fss mss css peb cob &gran

0 (m) cl

10

8

7

9

7

6

8

6

5

7

5

4

6

4

3

3

3

2

2

2

1

1

Sample ZC-32

0 (m) cl

si

fss mss css peb cob &gran

0 (m) cl

si

fss mss css peb cob &gran

fss mss css peb cob &gran

Northeast Huanglonggou Spot 5 (K1 y)

East Huanglonggou Spot 4 (K1 y)

8

1

si

0 (m) cl

si

fss mss css peb cob &gran

Load structure

Undulate fold

Normal fault

Ripple mark

Plunged sediment mixtures

Dome-trough

Graded fault

Cross bedding

Diapir

Seimic unconformity

Liquified breccia

Inclined bedding

Dinosaur track

Dinosaur skeleton fossil

Table 1. Analytical data for U-Pb dating of detrital zircon - Sample ZC-32 S p ot s

Element （ppm) P b

T h

U

T h / U r at i o

Isotopic ratios 207

P

b/20 6 Pb

1 σ

207

Pb/

Age（Ma） 1 σ

206

Pb/

235

238

U

U

1 σ

207

P

b/20 6 Pb

1 σ

235

238

U

U

C on 1 c σ （ ％ ）

207

Pb/

1 206 σ Pb/

A g e ( M a )

E rr o r

1

3 1 0

4 5 8

4 2 2

1. 0 9

0.0 491

0. 0 0 0 2

0.1 35 8

0. 0 0 0 8

0.0 20 1

0. 0 0 0 1

150

1 1

12 9

1 12 8

0 10 1

1 2 8

0

2

1 5 3 5

4 9 6

3 1 5

1. 5 7

0.0 639

0. 0 0 0 3

1.1 05 5

0. 0 0 5 6

0.1 25 5

0. 0 0 0 4

737

9

75 6

3 76 2

2 99

7 6 2

2

3

3 1 4

5 5 4

3 1 1

1. 7 8

0.0 531

0. 0 0 2 5

0.1 46 8

0. 0 0 8 1

0.0 20 0

0. 0 0 0 2

332

1 0 7

13 9

7 12 8

1 10 9

1 2 8

1

4

6 2 1

1 1 2 9

7 0 0

1. 6 1

0.0 493

0. 0 0 0 3

0.1 37 0

0. 0 01 1

0.0 20 1

0. 0 0 0 1

161

2 1

13 0

1 12 9

0 10 1

1 2 9

0

5

2 4 8

5 1 1

5 1 2

1. 0 0

0.0 488

0. 0 0 0 2

0.1 34 3

0. 0 0 0 7

0.0 19 9

0. 0 0 0 1

139

1 1

12 8

1 12 7

0 10 0

1 2 7

0

6

1 5 1

2 6 4

1 5 1

1. 7 5

0.0 523

0. 0 0 2 1

0.1 44 4

0. 0 0 6 4

0.0 20 0

0. 0 0 0 1

302

9 3

13 7

6 12 7

1 10 7

1 2 7

1

7

2 6 2

2 8 1

1 0 3

2. 7 2

0.1 643

0. 0 0 1 4

0.5 50 3

0. 0 0 5 7

0.0 24 3

0. 0 0 0 1

250 2

1 5

44 5

4 15 5

1 28 8

1 5 5

1

8

3 0 3

5 7 4

3 6 5

1. 5 7

0.0 533

0. 0 0 0 7

0.1 52 5

0. 0 0 2 1

0.0 20 8

0. 0 0 0 1

339

3 0

14 4

2 13 3

0 10 9

1 3 3

0

9

7 9

2 7 4

2 4 1

1. 1 3

0.0 440

0. 0 0 0 6

0.1 22 1

0. 0 0 2 5

0.0 21 9

0. 0 0 0 9

err or

e r r o r

117 2 14 0

6 84

1 4 0

6

1 0

4 2 9

8 7 2

7 7 0

1. 1 3

0.0 487

0. 0 0 0 2

0.1 32 5

0. 0 0 0 8

0.0 19 8

0. 0 0 0 1

132

1 3

12 6

1 12 6

0 10 0

1 2 6

0

1 1

7 0 4

1 6 4 7

2 3 9

6. 8 9

0.0 499

0. 0 0 2 0

0.1 33 3

0. 0 0 6 2

0.0 19 3

0. 0 0 0 1

191

9 2

12 7

6 12 3

1 10 3

1 2 3

1

1 2

3 0 4 4

1 2 8 9

1 4 1 1

0. 9 1

0.1 107

0. 0 0 0 9

0.9 55 8

0. 0 0 5 5

0.0 62 8

0. 0 0 0 3

181 1

1 5

68 1

3 39 3

2 17 4

3 9 3

2

1 3

1 5 4 6

2 7 4 8

7 7 6

3. 5 4

0.0 994

0. 0 0 0 6

0.3 08 2

0. 0 0 2 9

0.0 22 5

0. 0 0 0 1

161 3

1 8 8

27 3

2 14 3

1 19 0

1 4 3

1

1 4

2 3 3

4 7 5

1 9 4

2. 4 5

0.0 495

0. 0 0 0 4

0.1 39 3

0. 0 0 1 3

0.0 20 4

0. 0 0 0 1

172

2 0

13 2

1 13 0

0 10 2

1 3 0

0

1 5

1 0 2 9

2 2 3 5

1 1 4 6

1. 9 5

0.0 511

0. 0 0 0 2

0.1 46 9

0. 0 0 0 7

0.0 20 9

0. 0 0 0 1

256

9

13 9

1 13 3

0 10 5

1 3 3

0

1 6

3 4 0

7 6 9

7 5 8

1. 0 1

0.0 467

0. 0 0 0

0.1 33 9

0. 0 0 5

0.0 20 6

0. 0 0 0

35

1 8

12 8

5 13 1

4 97

1 3 1

4

3

1

6

1 7

2 1 3

5 2 4

1 8 6

2. 8 2

0.0 491

0. 0 0 0 4

0.1 35 8

0. 0 0 1 2

0.0 20 0

0. 0 0 0 1

154

1 2

12 9

1 12 8

0 10 1

1 2 8

0

1 8

5 7 1

6 0 8

4 5 4

1. 3 4

0.0 512

0. 0 0 0 2

0.3 31 1

0. 0 0 1 8

0.0 46 9

0. 0 0 0 2

256

9

29 0

1 29 6

1 98

2 9 6

1

1 9

4 0 7

9 7 2

6 6 3

1. 4 7

0.0 500

0. 0 0 0 2

0.1 43 4

0. 0 0 0 9

0.0 20 8

0. 0 0 0 1

195

1 1

13 6

1 13 3

1 10 2

1 3 3

1

2 0

1 3 1 1

2 1 4

3 7 4

0. 5 7

0.1 289

0. 0 0 0 4

5.0 94 4

0. 0 2 4 6

0.2 86 8

0. 0 01 1

208 3

6

18 35

4 16 25

6 12 8

2 0 8 3

6

2 1

3

2 2 3

1 5 3

1. 4 6

0.0 485

0. 0 0 0 9

0.1 28 1

0. 0 0 2 5

0.0 19 2

0. 0 0 0 1

124

4 4

12 2

2 12 2

1 10 0

1 2 2

1

2 2

9 0 1

2 6 3

2 9 3

0. 9 0

0.0 691

0. 0 0 0 2

1.4 27 7

0. 0 0 7 3

0.1 49 8

0. 0 0 0 7

902

4

90 1

3 90 0

4 10 0

9 0 0

4

2 3

9 3 6

1 4 6

2 3 0

0. 6 4

0.1 170

0. 0 0 2 4

2.1 94 9

0. 0 5 3 1

0.1 34 9

0. 0 0 0 7

191 0

3 8

117 1 81 9 7 6

4 23 4

8 1 6

4

2 4

1 8 3 0

5 6 0

2 4 3

2. 3 0

0.0 658

0. 0 0 0 2

1.0 91 7

0. 0 0 8 9

0.1 20 3

0. 0 0 0 9

120 0

7

74 9

4 73 2

5 10 2

7 3 2

5

2 5

7 5 4

5 8 4

5 0 9

1. 1 5

0.1 294

0. 0 0

0.3 95 4

0. 0 1

0.0 21 8

0. 0 0

210 0

4 8

33 8

9 13 9

1 24 3

1 3 9

1

3 6

2 9 0. 0 0 1 0

0 1 0. 0 0 0 1

128

8

12 4

1 12 4

1 10 0

1 2 4

1

0. 0 0 2 3

256 3

2

24 90

5 24 01

1 10 0 7

2 5 6 3

2

0.0 19 7

0. 0 0 0 1

132

1 5

12 6

1 12 6

1 10 0

1 2 6

1

0. 0 0 7 3

0.1 13 4

0. 0 0 0 7

866

7

73 5

4 69 3

4 10 6

6 9 3

4

0.1 35 0

0. 0 0 1 4

0.0 19 9

0. 0 0 0 2

165

2 1

12 9

1 12 7

1 10 1

1 2 7

1

0. 0 0 0 7

0.1 37 4

0. 0 0 2 3

0.0 20 0

0. 0 0 0 2

187

2 7

13 1

2 12 8

2 10 2

1 2 8

2

0.0 589

0. 0 0 0 3

0.5 77 7

0. 0 0 5 6

0.0 71 1

0. 0 0 0 5

565

1 1

46 3

4 44 2

3 10 5

4 4 2

3

2. 5 1

0.0 500

0. 0 0 0 2

0.1 38 2

0. 0 0 1 2

0.0 20 0

0. 0 0 0 1

195

1 4

13 1

1 12 8

1 10 3

1 2 8

1

1. 3

0.0 497

0. 0

0.1 37

0. 0

0.0 20

0. 0

189

1 7

13 0

1 12 8

1 10 2

1 2

1

0.0 19 4

2 6

3 1 4

5 7 2

3 1 6

1. 8 1

0.0 486

0. 0 0 0 3

0.1 29 8

2 7

3 7 4 1

3 2 3

1 3 0

2. 4 8

0.1 705

0. 0 0 0 3

10. 61 30

0. 0 5 7 1

0.4 51 4

2 8

1 2 8

2 6 9

2 8 0

0. 9 6

0.0 487

0. 0 0 0 3

0.1 31 9

0. 0 0 1 0

2 9

1 7 2 8

5 5 5

5 9 0

0. 9 4

0.0 679

0. 0 0 0 2

1.0 62 7

3 0

6 5

1 4 4

1 1 7

1. 2 3

0.0 493

0. 0 0 0 4

3 1

1 4 5

2 7 3

1 3 0

2. 0 9

0.0 499

3 2

3 7 0

2 0 3

1 4 3

1. 4 2

3 3

6 2 2

1 3 4 3

5 3 4

3 4

1 3

2 8

2 2

8

0 0 4

0

0 1 2

0

0 0 1

0.2 749

0. 0 0 5 0

13. 99 20

0. 3 7 2 9

0.3 65 5

0. 0 0 4 7

333 4

2 8

27 49

2 20 5 08

2 16 2 6

3 3 3 4

2 8

2. 3 0

0.0 488

0. 0 0 0 3

0.1 34 6

0. 0 01 1

0.0 20 0

0. 0 0 0 1

200

1 5

12 8

1 12 8

1 10 0

1 2 8

1

1 6 9

1. 7 1

0.0 504

0. 0 0 0 4

0.1 39 4

0. 0 0 1 3

0.0 20 1

0. 0 0 0 1

213

2 0

13 2

1 12 8

1 10 3

1 2 8

1

9 2

1 1 9

0. 7 7

0.1 670

0. 0 0 0 3

11. 11 90

0. 0 5 8 8

0.4 82 8

0. 0 0 2 3

252 7

4

25 33

5 25 40

1 10 0 0

2 5 2 7

4

4 8 2

1 1 6 5

9 5 9

1. 2 1

0.0 503

0. 0 0 0 4

0.1 41 7

0. 0 01 1

0.0 20 4

0. 0 0 0 1

209

2 1

13 5

1 13 0

1 10 3

1 3 0

1

4 0

2 6 1

6 0 8

4 5 0

1. 3 5

0.0 524

0. 0 0 0 3

0.1 44 9

0. 0 0 0 9

0.0 20 1

0. 0 0 0 1

302

1 1

13 7

1 12 8

1 10 7

1 2 8

1

4 1

1 2 2 7

2 0 9 2

1 2 7 3

1. 6 4

0.0 936

0. 0 0 1 4

0.2 86 3

0. 0 0 4 6

0.0 22 2

0. 0 0 0 1

150 2

2 8

25 6

4 14 1

1 18 1

1 4 1

1

4 2

1 5 9

3 7 8

1 4 0

2. 7 0

0.0 514

0. 0 0 0 4

0.1 47 3

0. 0 0 1 4

0.0 20 8

0. 0 0 0 1

257

1 9

14 0

1 13 3

1 10 5

1 3 3

1

4

5

8

3

2.

0.0

0.

0.1

0.

0.0

0.

235

1

15

1 15

1 10

1

1

4

6

0

0

3 5

3 6 1 6

2 4 6

1 3 5

1. 8 2

3 6

2 5 6

5 7 5

2 5 0

3 7

1 3 8

2 8 9

3 8

8 4 9

3 9

3

2 9

3 2

4 9

509

0 0 0 4

67 5

0 0 1 6

23 9

0 0 0 1

7

7

2

3

5 2

4 5

3 4 7

7 3 1

1 9 9

3. 6 7

0.0 825

0. 0 0 0 9

0.2 45 8

0. 0 0 3 0

0.0 21 6

0. 0 0 0 2

125 7

2 1

22 3

2 13 8

1 16 2

1 3 8

1

4 6

2 1 9

4 2 0

4 2 3

0. 9 9

0.0 566

0. 0 0 0 4

0.1 66 3

0. 0 0 1 6

0.0 21 3

0. 0 0 0 2

476

1 9

15 6

1 13 6

1 11 5

1 3 6

1

4 7

7 1 2 7

1 1 2 3 5

3 4 1 8

3. 2 9

0.1 792

0. 0 0 1 0

0.5 10 7

0. 0 0 3 0

0.0 20 7

0. 0 0 0 1

264 6

1 0

41 9

2 13 2

1 31 7

1 3 2

1

4 9

2 4 8 9

4 8 5 4

1 1 4 1

4. 2 6

0.1 148

0. 0 0 5 5

0.3 73 2

0. 0 2 3 0

0.0 22 3

0. 0 0 0 2

187 7

8 7

32 2

1 14 7 2

1 22 6

1 4 2

1

5 1

1 1 9 5

2 3 6 0

7 6 5

3. 0 8

0.0 933

0. 0 0 1 2

0.2 62 2

0. 0 0 4 7

0.0 20 4

0. 0 0 0 3

149 4

8

23 6

4 13 0

2 18 1

1 3 0

2

5 2

1 5 3

4 7

2 6

1. 8 1

0.0 717

0. 0 0 0 7

1.5 72 8

0. 0 2 9 8

0.1 59 7

0. 0 0 2 8

977

1 5

96 0

1 95 2 5

1 10 5 0

9 5 5

1 5

5 3

2 2 4 9

3 3 8

4 9 2

0. 6 9

0.2 750

0. 0 1 0 1

4.9 66 5

0. 0 3 4 7

0.1 45 2

0. 0 0 5 2

333 5

5 7

18 14

6 87 4

2 38 9 1

8 7 4

2 9

5 4

1 6 9

3 6 7

1 5 0

2. 4 4

0.0 521

0. 0 0 1 2

0.1 51 9

0. 0 0 4 7

0.0 21 1

0. 0 0 0 4

287

5 6

14 4

4 13 5

2 10 6

1 3 5

2

5 5

1 0 1

2 8 5

1 3 9

2. 0 5

0.1 337

0. 0 0 2 0

0.4 10 1

0. 0 0 8 0

0.0 22 2

0. 0 0 0 2

214 7

2 6

34 9

6 14 1

1 24 7

1 4 1

1

5 6

3 1 5

1 6 6

1 0 2

1. 6 3

0.0 832

0. 0 0 0 6

1.2 34 3

0. 0 1 8 9

0.1 07 6

0. 0 0 1 4

127 6

1 3

81 6

9 65 9

8 12 4

6 5 9

8

5 7

1 2 8

5 2 5

3 6 6

1. 4 3

0.0 487

0. 0 0 0 3

0.1 32 3

0. 0 0 1 2

0.0 19 7

0. 0 0 0 1

200

1 5

12 6

1 12 6

1 10 0

1 2 6

1

5 8

1 4 5

7 1 1

2 1 9

3. 2 6

0.0 486

0. 0 0 0 3

0.1 28 1

0. 0 01 1

0.0 19 1

0. 0 0 0 1

128

1 7

12 2

1 12 2

1 10 0

1 2 2

1

6 2

8 9

5 5 5

5 6 0

0. 9 9

0.0 479

0. 0 0 0 2

0.1 34 1

0. 0 0 1 0

0.0 20 3

0. 0 0 0 1

95

1 1

12 8

1 13 0

1 99

1 3 0

1

6 3

1 2 6

7 7 9

2 0 4

3. 8 2

0.0 483

0. 0 0 0 8

0.1 30 6

0. 0 0 3 4

0.0 19 4

0. 0 0 0 2

122

3 9

12 5

3 12 4

1 10 1

1 2 4

1

6 4

5 7

2 5 6

1 2 1

2. 1 1

0.0 570

0. 0 0 3 2

0.1 62 1

0. 0 1 0 4

0.0 20 6

0. 0 0 0 3

494

1 2 2

15 3

9 13 1

2 11 6

1 3 1

2

6 5

1 0 1 6

3 1 2

4 4 9

0. 7 0

0.1 425

0. 0 0 0 5

5.7 31 2

0. 0 3 0 9

0.2 92 0

0. 0 0 1 2

225 7

7

19 36

5 16 52

6 13 7

2 2 5 7

7

6 6

4 3 7

1 1 1 6

8 9 1

1. 2 5

0.0 501

0. 0 0 0

0.2 74 5

0. 0 0 2

0.0 39 8

0. 0 0 0

198

1 5

24 6

2 25 2

1 98

2 5 2

1

3

0

2

6 9

2 2 2

6 3 8

2 5 3

2. 5 2

0.1 188

0. 0 0 1 4

0.3 52 4

0. 0 0 4 6

0.0 21 5

0. 0 0 0 1

193 9

2 1

30 7

3 13 7

1 22 3

1 3 7

1

7 0

2 9 4 3

6 3 2

3 6 6

1. 7 3

0.1 805

0. 0 0 0 8

10. 50 60

0. 0 6 4 8

0.4 22 4

0. 0 0 1 7

265 7

7

24 80

6 22 71

8 11 7

2 6 5 7

7

7 1

9 8 0

1 7 1

1 1 3

1. 5 1

0.1 855

0. 0 0 0 9

12. 01 80

0. 1 0 3 5

0.4 70 2

0. 0 0 3 3

270 3

1 4

26 06

8 24 84

1 10 4 9

2 7 0 3

1 4

7 2

2 6 0 8

1 9 0 5

7 2 6

2. 6 2

0.0 749

0. 0 0 0 4

1.1 15 9

0. 0 0 9 3

0.1 08 0

0. 0 0 0 4

106 5

1 1

76 1

4 66 1

3 11 5

6 6 1

3

7 5

1 2 2 3

5 7 4 0

2 0 6 4

2. 7 8

0.0 485

0. 0 0 0 2

0.1 31 2

0. 0 0 0 7

0.0 19 6

0. 0 0 0 1

124

4 2

12 5

1 12 5

0 10 0

1 2 5

0

7 6

3 2 4

1 3 5 6

6 7 3

2. 0 1

0.0 590

0. 0 0 0 4

0.1 64 4

0. 0 0 1 2

0.0 20 2

0. 0 0 0 1

565

1 9

15 5

1 12 9

0 12 0

1 2 9

0

7 7

3 8 1 7

2 7 8 7

1 1 5 5

2. 4 1

0.1 771

0. 0 0 0 9

2.6 33 4

0. 0 2 4 0

0.1 08 2

0. 0 0 1 0

262 6

9

13 10

7 66 2

6 39 6

6 6 2

6

7 8

3 1 1

2 3 9

1 3 8

1. 7 3

0.0 651

0. 0 0 0 2

1.1 35 7

0. 0 0 5 8

0.1 26 6

0. 0 0 0 5

789

6

77 0

3 76 8

3 10 0

7 6 8

3

7 9

4 5 1

1 7 3

1 9 0

9. 1 4

0.1 783

0. 0 0

0.5 76 3

0. 01 1

0.0 23 3

0. 0 0

263 9

6 3

46 2

8 14 9

1 31 1

1 4 9

1

0

6 0

0

3 2

8

8 0

2 3 4

1 2 7 0

7 8 3

1. 6 2

0.0 486

0. 0 0 0 2

0.1 28 7

0. 0 0 0 8

0.0 19 2

8 1

7 1 5

2 6 0 0

7 0 5

3. 6 9

0.1 155

0. 0 0 3 0

0.3 39 8

0. 0 0 9 7

0.0 21 2

8 2

3 7

1 6 1

1 3 8

1. 1 7

0.0 485

0. 0 0 0 4

0.1 23 4

0. 0 0 1 3

8 3

1 0 1

4 7 2

4 8 6

0. 9 7

0.0 486

0. 0 0 0 2

0.1 31 2

8 4

1 0 7

3 8 2

1 9 2

1. 9 9

0.0 736

0. 0 0 0 8

8 5

1 3 0 8

3 3 3

3 5 6

0. 9 3

0.1 518

8 6

3 6 8

1 5 3 5

2 6 0

5. 9 1

8 7

1 2 0

3 1 9

5 9

8 8

5 4

1 3

7 6

0 1 0. 0 0 0 1

132

1 1

12 3

1 12 3

1 10 0

1 2 3

1

0. 0 0 0 1

188 8

5 2

29 7

7 13 5

1 22 0

1 3 5

1

0.0 18 4

0. 0 0 0 1

124

2 2

11 8

1 11 8

1 10 0

1 1 8

1

0. 0 0 0 8

0.0 19 6

0. 0 0 0 1

128

1 1

12 5

1 12 5

0 10 0

1 2 5

0

0.2 08 6

0. 0 0 2 4

0.0 20 5

0. 0 0 0 1

103 1

2 1

19 2

2 13 1

1 14 7

1 3 1

1

0. 0 0 0 8

5.2 40 2

0. 0 2 1 6

0.2 51 0

0. 0 0 1 6

236 6

9

18 59

4 14 43

8 16 4

2 3 6 6

9

0.0 485

0. 0 0 0 3

0.1 26 7

0. 0 0 0 9

0.0 19 0

0. 0 0 0 1

124

4 5

12 1

1 12 1

1 10 0

1 2 1

1

5. 3 7

0.1 812

0. 0 0 6 2

0.5 96 9

0. 0 2 6 7

0.0 23 0

0. 0 0 0 2

266 5

5 7

47 5

1 14 7 6

2 32 5

1 4 6

2

1. 7

0.1 005

0. 0

0.2 95

0. 0

0.0 21

0. 0

163 3

4 4

26 3

6 13 6

1 19 4

1 3

1

0 8 1 0. 0 0 1 0

3

5.2 21 7

0. 0 6 1 7

0.2 30 8

0. 0 0 2 7

0.1 77 5

0. 0 0 8 2

0.0 496

0. 0 0 0 3

0.1 38 5

1. 0 3

0.1 375

0. 0 0 0 4

1 3 3

0. 7 5

0.0 660

5 4 3

2. 4 6

0.0 531

0 2 4

8

0.0 487

0. 0 0 0 2

0.1 31 2

0. 5 8

0.1 681

0. 0 0 3 8

1 5 8

2. 1 5

0.0 618

6 0 3

3 1 3

1. 9 3

9 9 3

1 5 9

1 5 5

9 9

1 9 8

9 9

1 0 0

3 8 5

1 3 3 7

3

3 7

3

5

8 9

2 0 2

6 7 1

4 1 5

1. 6 2

9 2

1 0 2 9

2 0 7

3 5 5

9 3

1 3 6

3 3 9

9 6

1 9 4

9 7

0 0 2 0. 0 0 0 1

6

200

1 1

12 5

1 12 5

1 10 0

1 2 5

1

0. 0 0 4 2

253 9

3 8

18 56

1 13 0 39

2 19 2 0

2 5 3 9

3 8

0.0 20 8

0. 0 0 0 2

665

9 9

16 6

7 13 3

1 12 5

1 3 3

1

0. 0 0 1 3

0.0 20 3

0. 0 0 0 2

176

1 5

13 2

1 12 9

1 10 2

1 2 9

1

7.2 59 8

0. 0 9 5 8

0.3 82 8

0. 0 0 5 0

219 6

6

21 44

1 20 2 89

2 10 3 5

2 1 9 6

6

0. 0 0 0 3

1.1 68 3

0. 0 0 8 8

0.1 28 3

0. 0 0 0 9

809

9

78 6

4 77 8

5 10 1

7 7 8

5

0. 0 0 0 3

0.1 42 2

0. 0 0 1 4

0.0 19 4

0. 0 0 0 1

332

1 5

13 5

1 12 4

1 10 9

1 2 4

1

0.0 19 5

Table 2. Analytical data for U-Pb dating of detrital zircon - Sample ZC-4 Th Isotopic ratio S Element Age（Ma） p （ppm） /U o P T U rat 207 1 207 1 206 1 207 1 207 1 206 io Pb/ σ Pb σ Pb σ Pb/ σ Pb σ Pb ts b h 206 206 /23 /23 /23 /23 5 8 5 8 U U U U Pb Pb

Co nc 1 （ σ ％ ）

Ag e ( M a)

E r r o r

1

5 0

1 0 0

9 2

1. 09

0.0 54 1

0. 0 0 1 6

0.1 19 6

0. 0 0 4 1

0.0 16 0

0. 0 0 0 3

37 6

6 9

11 5

4

10 2

2

11 2

10 2

2

2

4 6

5 1

5 1

0. 99

0.1 67 0

0. 0 0 4 1

0.4 66 4

0. 0 1 0 6

0.0 20 9

0. 0 0 0 5

25 28

4 1

38 9

7

13 3

3

29 2

13 3

3

3

3 7

7 4

4 4

1. 68

0.0 49 0

0. 0 0 2 2

0.1 27 6

0. 0 0 7 6

0.0 18 2

0. 0 0 0 5

14 6

1 0 6

12 2

7

11 6

3

10 5

11 6

3

4

1 0 5

2 3 5

2 7 2

0. 87

0.0 48 0

0. 0 0 0 4

0.1 24 2

0. 0 0 1 3

0.0 18 8

0. 0 0 0 1

98

1 9

11 9

1

12 0

1

99

12 0

1

5

1 1 6

2 3 7

2 7 1

0. 88

0.0 51 6

0. 0 0 0 5

0.1 38 0

0. 0 0 1 5

0.0 19 4

0. 0 0 0 1

26 5

1 6

13 1

1

12 4

1

10 6

12 4

1

6

6 9

1 3 1

1 8 6

0. 71

0.0 50 2

0. 0 0 0 7

0.1 36 0

0. 0 0 2 1

0.0 19 6

0. 0 0 0 1

21 1

3 1

12 9

2

12 5

1

10 3

12 5

1

7

7 9

1 2 0

1 7 6

0. 68

0.0 50 4

0. 0 0 0 0

0.1 37 3

0. 0 0 0 0

0.0 19 8

0. 0 0 0 0

21 3

0

13 1

0

12 6

0

10 3

12 6

0

8

1 1 8

2 3 6

2 7 5

0. 86

0.0 48 8

0. 0 0 0 5

0.1 28 7

0. 0 0 1 3

0.0 19 1

0. 0 0 0 1

13 9

2 2

12 3

1

12 2

1

10 1

12 2

1

9

1 5 5

3 1 0

2 7 4

1. 13

0.0 49 4

0. 0 0 0 6

0.1 28 0

0. 0 0 1 5

0.0 18 8

0. 0 0 0 1

16 5

2 8

12 2

1

12 0

1

10 2

12 0

1

1 0

1 2 3

2 8 5

1 4 0

2. 03

0.0 48 7

0. 0 0 1 0

0.1 29 1

0. 0 0 2 5

0.0 19 3

0. 0 0 0 1

13 2

5 3

12 3

2

12 3

1

10 0

12 3

1

1 1

1 4 2 8

5 1 4

8 1 2

0. 63

0.0 67 0

0. 0 5 9 6

0.6 29 0

0. 1 9 4 8

0.0 82 2

0. 0 0 5 8

83 7

1 2 1 4

49 5

1 2 2

50 9

3 5

97

50 9

3 5

1 2

3 1

5 8

5 7

1. 01

0.0 47 2

0. 0 0 1 2

0.1 21 0

0. 0 0 4 0

0.0 18 4

0. 0 0 0 3

58

5 9

11 6

4

11 7

2

99

11 7

2

1 3

9 2

2 0 2

2 1 3

0. 95

0.0 51 8

0. 0 0 0 6

0.1 29 6

0. 0 0 1 5

0.0 18 2

0. 0 0 0 1

28 0

2 6

12 4

1

11 6

1

10 7

11 6

1

1 5

5 6

1 4 0

1 2 6

1. 12

0.0 49 7

0. 0 0 0 8

0.1 31 4

0. 0 0 2 1

0.0 19 2

0. 0 0 0 1

18 9

3 7

12 5

2

12 3

1

10 2

12 3

1

1 7

1 9 3

4 3 5

3 2 9

1. 32

0.0 47 2

0. 0 0 0 4

0.1 22 6

0. 0 0 1 1

0.0 18 9

0. 0 0 0 1

58

1 9

11 7

1

12 0

1

97

12 0

1

1 8

3 3 3

7 7 1

5 4 9

1. 40

0.0 47 7

0. 0 0 0

0.1 22 5

0. 0 0 1

0.0 18 6

0. 0 0 0

83

2 0

11 7

1

11 9

1

98

11 9

1

4

4

1

1 9

7

1 1

1 4

0. 75

0.0 00 0

0. 0 0 0 0

1.1 70 6

0. 6 6 8 7

0.0 18 0

0. 0 1 1 4

err or

e r r o r

78 7

3 2 3

11 5

7 2

68 3

11 5

7 2

2 0

1 6 1

3 0 9

3 3 5

0. 92

0.0 47 7

0. 0 0 0 5

0.1 27 9

0. 0 0 1 6

0.0 19 5

0. 0 0 0 1

87

2 6

12 2

1

12 4

1

98

12 4

1

2 1

1 6 6

3 4 6

3 4 8

0. 99

0.0 47 5

0. 0 0 0 4

0.1 23 1

0. 0 0 1 5

0.0 18 8

0. 0 0 0 1

76

2 2

11 8

1

12 0

1

98

12 0

1

2 2

6 3

8 7

1 1 7

0. 75

0.0 49 6

0. 0 0 1 5

0.1 64 7

0. 0 0 4 3

0.0 24 3

0. 0 0 0 2

17 6

6 9

15 5

4

15 5

1

10 0

15 5

1

2 3

1 1 2

2 1 2

2 6 4

0. 80

0.0 51 4

0. 0 0 1 5

0.1 32 5

0. 0 0 3 9

0.0 18 8

0. 0 0 0 2

25 7

6 5

12 6

3

12 0

1

10 5

12 0

1

2 4

2 3 9

5 5 9

4 6 4

1. 20

0.0 47 2

0. 0 0 0 5

0.1 20 0

0. 0 0 1 5

0.0 18 5

0. 0 0 0 1

58

2 6

11 5

1

11 8

1

97

11 8

1

2 5

4 7

1 0 3

6 7

1. 54

0.0 46 1

0. 0 0 1 0

0.1 15 9

0. 0 0 2 9

0.0 18 3

0. 0 0 0 2

40 0

3 5 0

11 1

3

11 7

1

95

11 7

1

2 6

3 5 4

7 3 4

1 1 6 6

0. 63

0.0 49 2

0. 0 0 0 5

0.1 27 0

0. 0 0 2 0

0.0 18 8

0. 0 0 0 1

15 4

2 9

12 1

2

12 0

1

10 1

12 0

1

2 7

1 2 2

3 0 0

2 1 0

1. 43

0.0 54 1

0. 0 0

0.1 36 8

0. 0 0

0.0 18 4

0. 0 0

37 6

3 0

13 0

2

11 8

1

11 1

11 8

1

0 7

2 3

0 2

2 8

8 7

1 2 9

1 5 2

0. 84

0.0 50 6

0. 0 0 0 6

0.1 33 5

0. 0 0 2 2

0.0 19 2

0. 0 0 0 2

23 3

3 0

12 7

2

12 3

1

10 4

12 3

1

2 9

1 8

2 7

1 3

2. 15

0.2 98 5

0. 0 4 3 1

1.3 05 2

0. 8 4 2 0

0.0 30 0

0. 0 1 5 9

34 62

2 2 6

84 8

3 8 9

19 0

1 0 0

44 6

19 0

1 0 0

3 0

8 2

1 7 8

1 3 5

1. 32

0.0 48 4

0. 0 0 0 6

0.1 24 9

0. 0 0 2 2

0.0 18 8

0. 0 0 0 1

11 7

3 1

11 9

2

12 0

1

99

12 0

1

3 1

5 6

1 3 2

9 9

1. 34

0.0 50 1

0. 0 0 2 6

0.1 25 4

0. 0 0 6 6

0.0 18 2

0. 0 0 0 2

19 8

1 2 2

12 0

6

11 6

1

10 3

11 6

1

3 2

8 9

1 7 5

2 5 7

0. 68

0.0 52 4

0. 0 0 1 1

0.1 38 8

0. 0 0 3 3

0.0 19 3

0. 0 0 0 2

30 2

4 6

13 2

3

12 3

1

10 7

12 3

1

3 3

9 2

4 7

9 0

0. 53

0.0 58 8

0. 0 0 0 9

0.6 31 9

0. 0 1 2 6

0.0 78 5

0. 0 0 1 1

56 7

3 5

49 7

8

48 7

7

10 2

48 7

7

3 4

2 0 4

6 8

1 1 7

0. 58

0.0 63 9

0. 0 0 0 6

1.0 26 5

0. 0 1 2 7

0.1 17 0

0. 0 0 0 9

73 9

2 5

71 7

6

71 3

5

10 1

71 3

5

3 5

1 3

5 0

4 9

1. 03

0.0 50 6

0. 0 0 2 4

0.1 31 4

0. 0 0 6 3

0.0 18 9

0. 0 0 0 2

22 0

1 0 9

12 5

6

12 0

1

10 4

12 0

1

3 6

5 8

5 3

1 9

2. 78

0.4 07

0. 0

2.7 02

1. 9

0.0 52

0. 0

39 36

2 1

13 29

5 9

33 1

1 0

11 91

33 1

1 0

6

8

4

3

5 6 6

0

6 0 5

6

1 6 7

3 7

1 9 2

4 9 3

3 6 4

3 8

6 9

1 4 1

3 9

4 1

4 0

0

9

2

2

1. 36

0.0 48 8

0. 0 0 0 6

0.1 20 4

0. 0 0 1 6

0.0 18 0

0. 0 0 0 1

20 0

3 0

11 5

1

11 5

1

10 0

11 5

1

1 8 6

0. 76

0.0 52 5

0. 0 0 0 5

0.1 36 8

0. 0 0 1 7

0.0 18 9

0. 0 0 0 1

30 9

2 4

13 0

2

12 1

1

10 8

12 1

1

1 0 7

1 6 2

0. 66

0.0 48 7

0. 0 0 1 0

0.1 33 1

0. 0 0 2 8

0.0 19 9

0. 0 0 0 2

13 2

5 3

12 7

3

12 7

1

10 0

12 7

1

5 8

9 0

5 9

1. 54

0.0 57 4

0. 0 1 1 0

0.1 56 4

0. 0 3 3 1

0.0 19 4

0. 0 0 0 2

50 6

4 3 0

14 8

2 9

12 4

1

11 9

12 4

1

4 1

3 5 6

3 1

5 5

0. 56

0.1 63 3

0. 0 0 0 6

10. 66 97

0. 1 0 1 7

0.4 74 3

0. 0 0 4 2

24 90

6

24 95

9

25 03

1 9

99

24 90

6

4 3

1 7 7

3 9 1

3 7 3

1. 05

0.0 48 1

0. 0 0 0 4

0.1 27 7

0. 0 0 1 2

0.0 19 3

0. 0 0 0 1

10 6

1 7

12 2

1

12 3

1

99

12 3

1

4 4

3 5 4

8 9 1

4 3 3

2. 06

0.0 49 5

0. 0 0 0 3

0.1 32 3

0. 0 0 1 1

0.0 19 4

0. 0 0 0 1

17 2

1 2

12 6

1

12 4

1

10 2

12 4

1

4 5

9 2

2 1 3

1 5 4

1. 38

0.0 49 1

0. 0 0 0 6

0.1 27 6

0. 0 0 1 7

0.0 18 9

0. 0 0 0 1

15 0

2 6

12 2

2

12 1

1

10 1

12 1

1

4

9

1

2

0.

0.0

0.

0.1

0.

0.0

0.

21

3

12

2

11

1

10

11

1

6

2

9 5

2 5

87

50 1

0 0 0 7

29 9

0 0 2 8

18 7

0 0 0 2

1

1

4

9

4

9

4 7

4 0 2

9 0 2

6 5 4

1. 38

0.0 50 4

0. 0 0 0 6

0.1 36 1

0. 0 0 2 5

0.0 19 6

0. 0 0 0 2

21 3

3 0

13 0

2

12 5

1

10 4

12 5

1

4 8

5 6

1 1 9

1 5 5

0. 77

0.0 48 7

0. 0 0 0 5

0.1 25 7

0. 0 0 1 5

0.0 18 7

0. 0 0 0 1

20 0

2 6

12 0

1

12 0

1

10 1

12 0

1

4 9

2 2 3

4 9 0

2 2 3

2. 19

0.0 46 9

0. 0 0 0 4

0.1 24 5

0. 0 0 1 5

0.0 19 3

0. 0 0 0 1

43

2 2

11 9

1

12 3

1

97

12 3

1

5 0

1 4 6

3 1 4

3 9 9

0. 79

0.0 49 7

0. 0 0 0 3

0.1 32 6

0. 0 0 1 3

0.0 19 4

0. 0 0 0 2

18 9

1 5

12 6

1

12 4

1

10 2

12 4

1

5 1

6 9

1 7 2

1 1 0

1. 56

0.0 47 9

0. 0 0 1 1

0.1 05 9

0. 0 0 3 3

0.0 15 9

0. 0 0 0 3

95

5 6

10 2

3

10 1

2

10 1

10 1

2

5 2

1 4

3 1

3 3

0. 94

0.0 40 4

0. 0 0 6 2

0.1 10 7

0. 0 0 9 9

0.0 16 7

0. 0 0 0 7

err or

10 7

9

10 7

5

10 0

10 7

5

5 3

7 6

1 3 6

1 3 2

1. 03

0.0 50 9

0. 0 0 1 3

0.1 32 9

0. 0 0 3 7

0.0 18 9

0. 0 0 0 2

23 9

6 1

12 7

3

12 1

2

10 5

12 1

2

5 4

1 2 7

2 7 3

3 2 0

0. 85

0.0 47 9

0. 0 0 0 6

0.1 22 9

0. 0 0 1 6

0.0 18 6

0. 0 0 0 1

10 0

2 8

11 8

1

11 9

1

99

11 9

1

5 5

4 2

9 3

9 4

0. 99

0.0 42 4

0. 0 0 2 1

0.1 10 6

0. 0 0 4 8

0.0 19 1

0. 0 0 0 2

err or

e r r o r

10 7

4

12 2

2

88

12 2

2

5 6

2 4

7 7

9 3

0. 83

0.0 49 2

0. 0 0 3 0

0.1 28 4

0. 0 1 1 7

0.0 18 3

0. 0 0 0 2

15 4

1 4 7

12 3

1 1

11 7

1

10 5

11 7

1

5 7

6 7 0

6 8

4 1 5

0. 16

0.1 31 4

0. 0 0 1 2

4.2 54 4

0. 0 6 7 8

0.2 34 9

0. 0 0 3 3

21 16

1 5

16 85

1 3

13 60

1 7

15 6

21 16

1 5

5 8

5 8 4

1 3 3 1

5 6 5

2. 35

0.0 53 9

0. 0 0 0 8

0.1 39 9

0. 0 0 2 8

0.0 18 9

0. 0 0 0 3

36 5

3 3

13 3

2

12 0

2

11 0

12 0

2

5 9

4 5 7

1 6 0

1 8 2

0. 88

0.0 64 0

0. 0 0 0 3

1.0 03 4

0. 0 0 6 9

0.1 13 7

0. 0 0 0 7

74 3

3

70 6

4

69 4

4

10 2

69 4

4

6 0

4 8

5 0

8 9

0. 56

0.0 50 1

0. 0 0 0 6

0.2 68 8

0. 0 0 3 5

0.0 38 9

0. 0 0 0 3

21 1

2 9

24 2

3

24 6

2

98

24 6

2

6 1

3 6

8 8

9 2

0. 96

0.0 46 7

0. 0 0 1 1

0.1 07 6

0. 0 0 3 2

0.0 16 7

0. 0 0 0 3

35

6 5

10 4

3

10 7

2

97

10 7

2

6 2

1 3 7

2 5 8

2 6 9

0. 96

0.0 48 9

0. 0 0 0 6

0.1 43 2

0. 0 0 2 2

0.0 21 2

0. 0 0 0 1

14 6

2 7

13 6

2

13 5

1

10 0

13 5

1

6 3

1 1 4 8

1 1 6

7 8

1. 49

0.1 61 7

0. 0 0 0

10. 22 69

0. 0 7 9

0.4 58 5

0. 0 0 3

24 74

5

24 56

7

24 33

1 4

10 2

24 74

5

5

7

2

6 4

2 4 5

1 2 6

3 0 8

0. 41

0.0 55 3

0. 0 0 0 2

0.5 41 3

0. 0 0 3 4

0.0 70 9

0. 0 0 0 4

42 8

9

43 9

2

44 2

2

99

44 2

2

6 5

6 5

1 6 1

1 6 7

0. 96

0.0 47 7

0. 0 0 0 8

0.1 28 0

0. 0 0 2 4

0.0 19 5

0. 0 0 0 2

83

4 3

12 2

2

12 4

1

98

12 4

1

6 6

3 4 8

7 6 9

7 9 8

0. 96

0.0 46 6

0. 0 0 0 2

0.1 24 0

0. 0 0 0 8

0.0 19 3

0. 0 0 0 1

28

1 3

11 9

1

12 3

1

96

12 3

1

6 7

3 6 4

1 3 0

1 7 5

0. 74

0.0 63 5

0. 0 0 0 3

1.0 26 7

0. 0 0 6 7

0.1 17 3

0. 0 0 0 6

72 4

8

71 7

3

71 5

4

10 0

71 5

4

6 8

6 6 7

2 5 5

2 2 4

1. 14

0.0 63 4

0. 0 0 0 4

1.0 19 1

0. 0 0 9 2

0.1 16 6

0. 0 0 0 8

72 0

1 8

71 3

5

71 1

5

10 0

71 1

5

6 9

1 1 4

2 7 9

1 9 9

1. 40

0.0 51 0

0. 0 0 0 7

0.1 28 8

0. 0 0 1 8

0.0 18 4

0. 0 0 0 1

23 9

3 3

12 3

2

11 7

1

10 5

11 7

1

7 0

1 1 2

2 7 4

2 4 9

1. 10

0.0 49 5

0. 0 0 0 6

0.1 23 2

0. 0 0 1 7

0.0 18 1

0. 0 0 0 1

16 9

2 8

11 8

2

11 5

1

10 2

11 5

1

7 1

9 2

2 2 3

2 3 0

0. 97

0.0 48 2

0. 0 0 0 7

0.1 20 2

0. 0 0 2 1

0.0 18 1

0. 0 0 0 1

10 6

3 2

11 5

2

11 5

1

10 0

11 5

1

7 3

9

6 8

8 4

0. 81

0.0 50 8

0. 0 0

0.1 34 6

0. 0 0

0.0 19 2

0. 0 0

23 2

4 6

12 8

3

12 2

1

10 5

12 2

1

1 0

3 3

0 2

7 4

9 4

2 2 8

2 2 0

1. 03

0.0 48 0

0. 0 0 0 9

0.1 28 4

0. 0 0 2 8

0.0 19 4

0. 0 0 0 1

98

4 4

12 3

3

12 4

1

99

12 4

1

7 5

2 0

4 4

4 6

0. 96

0.0 47 3

0. 0 0 1 1

0.1 26 5

0. 0 0 3 2

0.0 19 4

0. 0 0 0 2

65

5 6

12 1

3

12 4

1

98

12 4

1

7 6

1 3 0

3 1 4

3 0 7

1. 02

0.0 47 4

0. 0 0 0 5

0.1 22 0

0. 0 0 1 3

0.0 18 6

0. 0 0 0 1

78

1 9

11 7

1

11 9

1

98

11 9

1

7 7

3 6

0

1

0. 00

0.4 31 2

0. 0 3 2 2

1.0 21 8

0. 8 9 6 0

0.0 16 9

0. 0 1 4 0

40 22

1 1 2

71 5

4 8 3

10 8

8 9

66 2

10 8

8 9

7 8

1 1 0

2 6 1

3 0 4

0. 86

0.0 49 3

0. 0 0 0 4

0.1 29 0

0. 0 0 1 2

0.0 19 0

0. 0 0 0 1

16 7

2 5

12 3

1

12 1

1

10 2

12 1

1

7 9

6

0

0

#D IV /0 !

0.0 91 4

0. 0 3 6 3

0.8 29 8

0. 3 3 7 9

0.0 05 9

0. 0 2 0 4

14 54

8 2 7

61 4

1 9 0

38

1 3 1

16 18

38

1 3 1

8 0

7

0

1

0. 57

0.2 17 9

0. 1 9 2 3

0.5 22 3

0. 6 1 0 0

0.0 06 1

0. 0 0 6 9

29 66

9 8 1

42 7

4 3 1

39

4 4

10 81

39

4 4

8 1

2 7 7

7 4 0

2 7 9

2. 65

0.0 46 2

0. 0 0 0 7

0.1 17 2

0. 0 0 1 9

0.0 18 4

0. 0 0 0 1

9

4 6

11 3

2

11 8

1

96

11 8

1

8 2

6 6

1 9

8 7

2. 19

0.0 50

0. 0

0.1 21

0. 0

0.0 17

0. 0

20 6

5 6

11 6

3

11 2

1

10 4

11 2

1

1

2

0 1 2

3

0 3 5

5

0 0 2

8 3

4 4 6

1 8 0

2 6 3

0. 68

0.0 64 0

0. 0 0 0 3

0.9 71 5

0. 0 0 6 7

0.1 10 0

0. 0 0 0 6

74 3

3

68 9

3

67 3

3

10 2

67 3

3

8 4

1 5

3 5

3 2

1. 08

0.0 53 5

0. 0 0 3 7

0.1 50 8

0. 0 1 2 4

0.0 19 3

0. 0 0 0 5

35 0

1 5 7

14 3

1 1

12 3

3

11 6

12 3

3

8 5

1 1 1

2 2 1

2 6 1

0. 85

0.0 46 7

0. 0 0 0 4

0.1 22 7

0. 0 0 1 3

0.0 19 1

0. 0 0 0 1

32

2 2

11 8

1

12 2

1

97

12 2

1

8 6

6 2

1 3 0

5 2

2. 49

0.0 46 5

0. 0 0 1 1

0.1 19 6

0. 0 0 3 1

0.0 18 6

0. 0 0 0 2

33

4 6

11 5

3

11 9

1

96

11 9

1

8 7

7 2

1 7 2

1 9 4

0. 88

0.0 47 5

0. 0 0 0 6

0.1 21 7

0. 0 0 1 7

0.0 18 6

0. 0 0 0 1

76

2 5

11 7

2

11 9

1

98

11 9

1

8 8

1 7

5 8

9 7

0. 60

0.0 50 0

0. 0 0 3 1

0.1 33 2

0. 0 0 8 8

0.0 19 2

0. 0 0 0 1

19 5

1 5 1

12 7

8

12 3

1

10 3

12 3

1

8 9

1 4 9

3 0 2

2 7 3

1. 11

0.0 78 2

0. 0 0 2 0

0.2 11 1

0. 0 0 5 9

0.0 19 5

0. 0 0 0 1

11 52

8 2

19 4

5

12 5

1

15 6

12 5

1

9 0

1 3 1

3 1 0

3 2 3

0. 96

0.0 49 2

0. 0 0 0 5

0.1 22 0

0. 0 0 1 5

0.0 18 0

0. 0 0 0 1

16 7

2 9

11 7

1

11 5

1

10 2

11 5

1

9

2

7

3

1.

0.0

0.

0.1

0.

0.0

0.

43

8

10

3

10

1

98

10

1

1

5

1

9

80

46 9

0 0 1 4

05 0

0 0 3 4

16 2

0 0 0 2

0

1

9 2

1 6 0

3 3 6

3 3 0

1. 02

0.0 47 8

0. 0 0 0 4

0.1 30 3

0. 0 0 1 3

0.0 19 8

0. 0 0 0 1

9 3

1 6 6

3 5 6

3 9 3

0. 91

0.0 47 1

0. 0 0 0 3

0.1 25 0

0. 0 0 1 1

0.0 19 3

9 4

1 3

3 6

3 9

0. 92

0.0 47 9

0. 0 0 1 2

0.1 23 1

0. 0 0 3 3

9 5

9 4

7 3

1 0 9

0. 67

0.0 53 8

0. 0 0 0 6

0.3 28 2

9 6

6 9

1 5 3

8 2

1. 88

0.0 67 2

0. 0 1 1 3

9 7

1 2 7

2 6 2

6 0 0

0. 44

0.0 48 6

9 8

5 7

1 1 7

3 5 3

0. 33

9 9

1 4 1

3 4 0

2 3 3

1. 46

4

4

87

1 4

12 4

1

12 6

1

98

12 6

1

0. 0 0 0 1

54

2 1

12 0

1

12 3

1

97

12 3

1

0.0 18 7

0. 0 0 0 1

10 0

6 1

11 8

3

11 9

1

99

11 9

1

0. 0 0 4 1

0.0 44 3

0. 0 0 0 3

36 1

2 4

28 8

3

27 9

2

10 3

27 9

2

0.1 74 3

0. 0 3 1 1

0.0 18 4

0. 0 0 0 1

85 6

3 5 6

16 3

2 7

11 7

1

13 9

11 7

1

0. 0 0 0 6

0.1 17 4

0. 0 0 1 6

0.0 17 6

0. 0 0 0 1

12 8

2 8

11 3

1

11 2

1

10 0

11 2

1

0.0 48 8

0. 0 0 0 4

0.1 16 4

0. 0 0 1 3

0.0 17 3

0. 0 0 0 1

13 9

2 3

11 2

1

11 0

1

10 1

11 0

1

0.0 47 2

0. 0 0 1 8

0.1 22 8

0. 0 0 5 1

0.0 18 6

0. 0 0 0 4

58

8 5

11 8

5

11 9

2

99

11 9

2

1 0 0

1 8 8

4 0 9

4 7 6

0. 86

0.0 48 7

0. 0 0 0 4

0.1 21 8

0. 0 0 1 4

0.0 18 1

0. 0 0 0 2

13 2

1 4

11 7

1

11 6

1

10 1

11 6

1

1 0 1

9 7 6

1 2 8

2 6 7

0. 48

0.1 13 2

0. 0 0 0 3

4.6 12 1

0. 0 2 8 7

0.2 95 5

0. 0 0 1 6

18 51

1

17 51

5

16 69

8

11 1

18 51

1

1 0 2

1 0 3 9

1 2 3

2 8 0

0. 44

0.1 40 2

0. 0 0 1 5

6.5 29 7

0. 4 2 2 8

0.3 46 7

0. 0 2 3 5

22 29

1 8

20 50

5 7

19 19

1 1 2

11 6

22 29

1 8

1 0 3

7 9

1 3 9

1 9 9

0. 70

0.0 49 4

0. 0 0 0 5

0.1 28 5

0. 0 0 2 1

0.0 18 8

0. 0 0 0 2

16 9

2 6

12 3

2

12 0

1

10 2

12 0

1

1 0 4

9 2 2

1 1 7

1 6 2

0. 72

0.1 22 4

0. 0 0 0 3

5.7 65 8

0. 0 6 1 1

0.3 41 4

0. 0 0 3 5

19 92

5

19 41

9

18 94

1 7

10 5

19 92

5

1 0 5

6 4 8

7 2 2

7 9 1

0. 91

0.0 50 9

0. 0 0 0 2

0.2 62 3

0. 0 0 2 9

0.0 37 4

0. 0 0 0 4

23 5

5

23 7

2

23 7

2

10 0

23 7

2

1 0 6

1 5 7

3 7 8

3 0 5

1. 24

0.0 49 7

0. 0 0 0 4

0.1 23 6

0. 0 0 1 7

0.0 18 0

0. 0 0 0 2

18 9

1 6

11 8

2

11 5

1

10 3

11 5

1

1 0 7

2 4

4 8

6 2

0. 78

0.0 48 5

0. 0 0 0 9

0.1 24 4

0. 0 0 2 4

0.0 18 7

0. 0 0 0 2

12 0

4 1

11 9

2

11 9

1

10 0

11 9

1

1 0 8

8 2

1 5 0

2 0 0

0. 75

0.0 49 3

0. 0 0 0

0.1 28 3

0. 0 0 1

0.0 18 9

0. 0 0 0

16 7

8

12 3

1

12 1

1

10 2

12 1

1

5

4

1

1 0 9

2 2 1

6 7 2

3 8 0

1. 77

0.0 47 0

0. 0 0 0 3

0.1 20 5

0. 0 0 1 0

0.0 18 6

0. 0 0 0 1

50

1 5

11 6

1

11 9

1

97

11 9

1

1 1 0

8 1

1 5 9

8 0

1. 99

0.1 24 1

0. 0 0 2 7

0.3 46 7

0. 0 0 8 1

0.0 20 2

0. 0 0 0 1

20 17

3 9

30 2

6

12 9

1

23 4

12 9

1

Highlights

►Soft-sediment deformation structures (SSDS) occur in dinosaur fossil beds of the Zhucheng depression, east China. ►The SSDS were likely triggered the paleo-earthquakes between 118-105 Ma and after 100 Ma. ►Massive dinosaur bone beds suggest burial by earthquake-triggered debris flows.