Nanjing University, China September , 20158–11

International Workshop on Climate and Environmental Evolution

in the Mesozoic Greenhouse World &

3rd IGCP 609 Workshop on Cretaceous Sea-Level Change

Cretaceous stratigraphy and sedimentology in southeastern China

FIELD TRIP GUIDE Xianghui Li, Wen Lai, Guang Hu, Shuzhong Shen, Xiumian Hu

TABLE OF CONTENTS

Introduction .............................................................................................................. 1

Day 1 (September 8th): Nanjing-Changxing-Jiande ................................... 6

Stop 1-1 The Pukou Formation, Upper Cretaceous ................................................. 6

Stop 1-2 The Chishan Formation, Upper Cretaceous .............................................. 7

Stop 1-3 The Meishan P/Tr GSSP Section ............................................................. 10

Day 2 (September 9th): Jiande-Guixi-Quzhou ............................................ 18

Stop 2-1 Intermountaine mollase facies, Hekou Formation of Guifeng Group,

Upper Cretaceous.................................................................................................... 18

Stop 2-2 Large-scale aeolian facies, Tangbian Formation of Guifeng Group, Upper

Cretaceous............................................................................................................... 20

Day 3 (September 10th): Quzhou-Longyou-Jiande-Shipu ...................... 23

Stop 3-1 Lacustrine facies, Jinhua Formation of Quzhou Group, Upper Cretaceous

................................................................................................................................ 23

Stop 3-2 Volcanic-sedimentary successions and paleosol facies of the Lower

Cretaceous Jiande Group ........................................................................................ 24

Day 4 (September 11th): Shipu-Nanjing ........................................................ 29

Stop 4-1 Transitional facies, Shipu Group, Lower Cretaceous .............................. 29

Reference .................................................................................................................. 34

Introduction

The South China block (SCB) consists of the Yangtze block to the northwest and the Cathaysian block to the southeast (Fig. 1). The present boundary between these two blocks is the northeasterly trending Jiang-Shao fault. The timing of the amalgamation between the Yangtze and Cathaysian blocks remains controversial. The predominant view was an early Neoproterozoic age for the amalgamation, ca. 900 to 880 Ma to ca. 800 Ma. During the Phanerozoic time, the south China block experienced four main tectonic events. 1) The Kwangsian orogeny, which is traditionally called the Chinese Caledonian orogeny, is characterized by the angular unconformity that separates the Devonian-Permian cover from strongly deformed pre-Devonian strata as well as syn-deformational metamorphism and subsequent anatexis. It is generally considered to be an early Paleozoic intracontinental orogen; 2) Late Paleozoic extensional rifting, which probably started in the Devonian; 3) the collision between South China and North China blocks during Middle to Late Triassic along the Su-Lu-Dabie-Qinling suture zones; 4) The Indosinian orogeny, which extended from the Late Permian to the Middle Triassic, was a result of the collision between the Indochina block and South China; 5) Late Mesozoic magmatism along the southeastern coast of South China, which represents an active continental margin.

Fig. 1. Sketch map of East China (Hu et al., 2012)

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The Cretaceous is an important period in geological time, and has also witnessed notable evolution and extinction of marine and terrestrial biotas. Among the most important and several issues faced by the international community are the greenhouse effects and global climate changes (Wan et al., 2007).

Cretaceous deposits are widespread in China. Most strata are of nonmarine origin, and marine sediments occur only in Tibet, western Tarim of Xinjiang, Taiwan and limited area of eastern Heilongjiang. The nonmarine deposits are outlined from northeast China, southeast China, southern interior China, southwest China, the Shaanxi-Gansu-Ningxia region, and northwestern China intermontane basins. The sedimentary facies and paleogeography are diversified (Wan et al., 2007).

Nonmarine Cretaceous strata in the coastal areas of southeastern China are quite different from those of northeastern China, and are composed mainly of volcanics, red beds and variegated deposits intercalated with evaporites at the top, which reach substantial thicknesses; coal is absent. The Lower-Upper Cretaceous boundary in this region has also been subject to varying interpretations, but recently-discovered fossils from the Chaochuan Formation in Zhejiang are known to be of the Cenomanian in the Hekou Formation of Fujian, thus the boundary in Zhejiang can be placed between the Chaochuan and Guantou formations. Another relatively complete nonmarine Cretaceous sequence, which includes 10 formations, has been established in this region (Wan et al., 2007).

During the Cretaceous, the continental interior of China was characterized by large lake systems in tectonic depressions and intermontane basins, with little or no marine influence. During the Cretaceous, most of southern China was characterized by very warm, dry climates, resulting in the deposition of extensive continental red beds, gypsum, and rock salt in large water-filled depressions and intermontane basins (Fig. 2, 3; Chen., 1987).

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Fig. 2. Sketch map showing the early Early Cretaceous (Neocomian) paleogeography in China (Chen., 1987). 1

=Tethys Sea. 2= Pacific Ocean. 3= Wusuli Gulf. 4= Shu Lake. 5 = Xichang Lake. 6 = Yunnan Lake. 7= Puer Lake. 8=

Ba Lake. 9 = Qingyang Lake. 10= ancient Datong River. 11= Chao Lake. 12= Junggar Basin. 13= Turpan Basin. 14=

Kuqa Basin. 15= unnamed River. 16= Kashi Gulf. 17= Songhua Lake. 18= Yunmeng Lake. 19= ancient Gan River.

20= ancient Fuchun River. 21 = active volcanic zones in the eastern coastal low land.

Fig. 3. Sketch map showing the early and middle Late Cretaceous (Cenomanian Santonian) paleogeography in

China (Chen., 1987). symbols same as in Fig. 2.

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A compilation of reliable isotopic age data indicates that Cretaceous magmatism in SE China (Fig. 4)occurred in four major episodes during 136–146 Ma, 122–129 Ma, 101–109 Ma and 87–97 Ma. A-type granitic and within-plate basaltic magmatism from 140–90 Ma suggests a dominant extensional environment in the region. Voluminous coeval high-K calc-alkaline rocks, which have geochemical features similar to those formed in continental back-arc and post-collision extension settings, are interpreted to have been generated in response to lithospheric extension. Cretaceous magmatism, NNE-trending wrench faulting and formation of extensional basin systems favour an extensional tectonic regime in SE China in the Cretaceous (Li., 2000).

Fig. 4. Sketch map showing the distribution of the Cretaceous volcanic rocks in SE China (Li., 2000).

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During the 4-day-excursion in southern Jiangsu, western Zhejiang and northeastern

Jiangxi provinces (Fig. 5, Table 1), we will visit the rocks and sections from Early

Cretaceous to Late Cretaceous. Major stops and attractions include: (1) Late Cretaceous

continental deposits of Chishan Formation and Pukou Formation (Jiangsu Province); (2)

the GSSP section of Permian-Triassic boundary in Meishan, Zhejiang Province; (3)

Cretaceous continental deposits in Jiangxi and Zhejiang Province; (4) shallow marine

deposits of Xiangshan Formation, Lower Cretaceous (Zhejiang Province).

Table 1. The table of Cretaceous regional stratigraphical correlation in southeast China

Epoch Nanjing Guixi Quzhou Jiande Shipu

K2 Chishan Fm. Lianhe Fm.

Quxian Fm. Fangyan Fm.

Pukou Fm. Tangbian Fm.

Hekou Fm. Jinhua Fm.

K1 Gecun Fm. Ganzhou Group

Zhongdai Fm.

Hengshan Fm.

Shipu Fm. Shouchang Fm.

Huobashan Group Huangjian Fm.

Laocun Fm.

Fig. 5. The sites of 3rd IGCP 609 workshop field excursion

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Day 1 (September 8th): Nanjing-Changxing-Jiande

Schedule:

8:00-8:40, Nanjing University to Yanziji Park

8:40-9:40, [Stop 1-1:Yanziji Park, Nanjing]. Investigating the Pukou Formation, Upper

Cretaceous

9:40-10:40, Yanziji Park to Chishan

10:40-11:40, [Stop 1-2:Chishan Mountain, Jurong]. Investigating the Chishan Formation,

Upper Cretaceous

11:40-12:40, lunch in Bus

11:40- 14:00, Chishan to GSSP Park, Changxing

14:00- 16:00, [Stop 1-3:GSSP Park, Changxing]. Investigating the Meishan P/Tr GSSP

Section.

16:00-19:30, Changxing to Jiande

19:30-, dinner and accommodation in the Kaiyue Hotel, Jiande City

Highlight: Pukou Formation and Chishan Formation (Upper Cretaceous sequences), the

Meishan P/Tr GSSP Section.

Stop 1-1 The Pukou Formation, Upper Cretaceous

Location: Yanziji Park, Nanjing city, Jiangsu province

Time: 1 hour

Background:

The Pukou Formation (K2p) of Upper Cretaceous has been deposited in Wangjing, Qianshan, Wuwei, Nanxuan, Changzhou, Jurong, Nanjing, Quanjiao, and Subei of the Lower Yangtze Region (Shang et al., 2002). The Pukou Formation covers unconformably on the Gecun Formation or the volcanic rock, and is possibly conformably covered by the Chishan Formation. The Gecun Formation is mainly composed of greyish-green siltstone and mudrocks.

The Pukou Formation (K2p) is composed of variable clastic lithologies, such as conglomerates, sandstone, siltstone, mudrocks, gypsum-salt rock. The lower part of the Pukou Formation is dominated by conglomerates, grayish purple vocanic conglomerates and sandstone. It deposited in fluvial fan environment. The upper part of the Pukou Formation is dominated by purple sandstone with siltstone or mudrocks, which may be replaced by mudrocks and gypsum-salt rock in some places. The upper part was interpreted to be

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deposited in outer fan and lacustrine facies in an arid climate environment (Jiangsu Geology and Mineral Resources Bureau, 1997).

The chronostratigraphy of the Pukou Formation is not well constrained due to lack of age-indicated fossils. Some isotopic ages on the igneous rocks from the Pukou Formation are mainly in the range of 70–120 Ma (Anhui Bureau of Geology and Mineral Resources, 1987, p. 263 Table 24, p. 312, 340; Jiangsu Bureau of Geology and Mineral Resources, 1984, p. 380, Table 2-1). Thus, the Pukou Formation is roughly inferred to be deposited in the Late Cretaceous according to the plant fossils Manica (Changlingia) Tholitoma, Classopllis, Monocolpopollentes, Sphaeripollenites, Lygodiumsporites, Cicatrcosisporites, Schizaeois- porites laevigataeformis (Jiangsu Geology and Mineral Resources Bureau, 1997).

Observation:

In the Yanziji Park, the southern bank of the Changjiang (Yangtze) River of Nanjing, large-scale conglomerates that were deposited by debris flow are well outcropped. Conglomerates are of gray-red, poorly sorted, poorly graded (Fig. 6).

Fig. 6. Photograph showing the large conglomerates of the Pukou Formation in fluvial fan environment

Stop 1-2 The Chishan Formation, Upper Cretaceous

Location: Chishan Mountain, Zhenjiang city, Jiangsu province

Time: 1 hour

Background:

The Chishan Formation (K2c) of Upper Cretaceous has been deposited in Zhenjiang, Nanjing of the Lower Yangtze Region. The Chishan Formation covers conformably on the Pukou

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Formation (Jiangsu Geology and Mineral Resources Bureau, 1997), and is unconformably covered by the Pliocene Basalt in Chishan area (Yue et al., 1997, Fig. 7).

Fig. 7. Geological map nearby Chishan Mountain (Yue et al., 1997)

The Chishan Formation (K2c) is composed of red sandstones, siltstones and mudrocks. The lower part of the Chishan Formation was interpreted to be deposited in lacustrine facies in arid-climate environment, but the upper part of the Chishan Formation was aeolian deposits with large-scale cross-bedding (Yue et al., 1997, Fig. 8).

The chronostratigraphy of the Chishan Formation is only roughly inferred to be Late Cretaceous according to the ostracoda (Cypridea-Cristocypridea-Eucypris) and the Charophyceae (Porochara-Euaclistochara-Mesochara) (He et al., 1981).

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Fig. 8 The sedimentary facie sequence of Chishan Formation in Chishan Mountain (Yue et al., 1997)

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Observation:

In the northeast of Chishan Mountain of Zhenjiang City, large-scale aeolian sandstones of the Chishan Formation are well outcropped at lots of quarries. Large cross-beddings can be readily observed, and the set of cross-bedding is astonishingly up to ca. 3 m thick (Fig. 9). Sandstones are of purple-red, well-sorted; medium to fine-grained with little suspension load.

Fig. 9. Late Cretaceous aeolian deposits of Chishan Formation in Jiangsu Province

Stop 1-3 The Meishan P/Tr GSSP Section

Location: the GSSP Geopark, Changxing county, Zhejiang province

Time: 2 hours

Background:

The Meishan Section D is located about 2 km southwest of the Meishan Town and the Meishan Section C is located about 300 m west to Section D (Fig. 10, 11).The geographical coordinates for the GSSPs of the Wuchiapingian-Changhsingian and Permian-Triassic boundaries are 31°4′55″N; 119°42′22.9″E and 31°4′50.47″N; 119°42′22.24″E. Meishan sections are well protected since 1980s and freely accessible for scientific researchers. The Meishan quarries (A-E, Z) were excavated to mine the limestone of the Changhsing Formation for cement, and Section D is in the middle of the quarried outcrops (Fig. 11)

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Fig. 10. Geological map nearby Meishan (Li et al., 2008).

Fig.11. Localities of Meishan sections A-E and Z (after Yin et al., 2001).

Upper Permian to lowest Triassic lithostratigraphical sequences at the Meishan Geopark:

The upper Permian to the lowest Triassic sequences at the Meishan Geopark are composed of the uppermost part of the Lungtan Formation, the Changhsing Formation and the Yinkeng Formation in ascending order (Fig. 12).

1) Lungtan Formation: This formation in the area is about 300 m thick. It is subdivided into 3 members (Fig. 12). The lower member (100 m thick) is mainly composed of coarse sandstones, siltstones and workable coal seams containing abundant Gigantopteris flora. The middle member (150 m thick) mainly consists of fine sandstones alternated with sandy mudstones containing abundant brachiopods, corals and fusulinids topped with a coal seam. The upper member (60 m thick) is composed of mudstones alternated with fine sandstones, containing abundant brachiopods and some ammonoids. The upper member is assigned to the late Wuchiapingian age, based on the presence of the ammonoids Konglingites and Jinjiangoceras and abundant Clarkina orientalis (Wang et al., 2006). Brachiopods are extremely abundant and diverse in the uppermost part of

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Lungtan Formation (Fig. 12). They are identical in composition with those from the Lopingian (Late Permian) in South China, as dominated by many common Lopingian species in South China including Spinomarginifera lopingensis(Kayser), Edriosteges poyangensis (Kayser), Orthothetina ruber (Frech), Cathaysia chonetoides (Chao), Haydenella kiangsiensis (Kayser) and Permophricodothyrisgrandis (Chao). Orthotetida and Productida are the two most diverse and abundant groups in the brachiopod fauna. In addition, an extremely abundant tiny chonetid, Neochonetes (Huangichonetes) meishanensis is present. A chonetid-like productid Cathaysia chonetoides, a large spiriferid species, Permophricodothyris elegantula, and an enteletid species, Enteletes retardata, are also very common in the brachiopod assemblage (Fig. 12). There are only a few small brachiopods including the tiny Neochonetes(Huangichonetes) meishanensisand Cathaysia chonetoides (Chao) continue to be present in the lowest part of the Changhsing Limestone.

2) Changhsing Formation: This formation is about 50 m thick. It is subdivided into two members (Fig. 12). The upper member (Meishan Member, about 11 m thick) is composed of dark gray median-bedded limestones, intercalated with cherty nodules, containing abundant conodonts, foraminifers and ammonods (such as Pleuronodoceras, Rotodiscoceras. etc.). The lower member (Baoqing Member, about 32 m thick) is composed of dark grayish median-bedded limestones, intercalated with a few cherty beds, containing abundant conodonts, foraminifers and ammonoids (such as Tapashanites, Mingyuexiaceras etc.). Additionally, a few shallow-water radiolarians and some brachiopods (e.g., Araxathyris) were discovered.

3) Yinkeng Formation: This formation is about 14 m thick at Meishan,and composed of dark gray thin-bedded calcareous mudstones and gray thin-bedded marls, both of them formed distinct rhythms (cycles).

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Fig.12. Lithological column of the uppermost Lungtan Formation and distribution of brachiopods at the Meishan

Section C (after Li et al., 2008).

Conodont zones from the uppermost Lungtan, Changhsing and Yinkeng formations

Conodonts are very abundant in the Changhsingian Stage at the Meishan sections and the conodont biostratigraphy together with geochronologic data provide a basic temporal framework to calibrate the end-Permian mass extinction and the global correlation.

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Nine conodont zones have been recognized from the uppermost Lungtan Formation, Changhsing Formation and Yinkeng Formation at the Meishan sections (Yin et al., 2001; Yuan et al., 2014), in ascending order, including:

1) Clarkina longicuspidata Zone, from beds 1 to 4a-1 of the uppermost Lungtan Formation (latest Wuchiapingian); 2) Clarkina wangi Zone, from beds 4a-2 to 10 (The FAD of C. wangi marked the beginning of the Changhsingian Stage); 3) Clarkina subcarinata Zone, from Bed 11 to the lower part of Bed 12; 4) Clarkina changxingensis Zone, from the upper part of Bed 12 to the lower part of Bed 22; 5) Clarkina yini Zone, from the upper part of beds 22 to 24d; 6) Clarkina meishanensis Zone, from beds 24e to 25; 7) Clarkina zhejiangensis–Hindeodus changxingensis Zone, from beds 26 to 27b; 8) Hindeodus parvus Zone, from beds 27c and 27d (FAD of H. parvus marked the beginning of the Triassic); 9) Isarcicella isarcica Zone, from Bed 28 and upwards.

Observation:

GSSP of the Wuchiapingian-Changhsingian boundary at the Meishan Section D

The GSSP for the Wuchiapingian-Changhsingian boundary was ratified by IUGS at Meishan Section D in 2006 (Jin et al., 2006). The boundary has been defined by the First Appearance Datum (FAD) of the conodont Clarkina wangi within the lineage from Clarkina longicuspidata to Clarkina wangi, at a point 88 cm above the base of the Changxing Limestone in the lower part of Bed 4 (base of 4a-2) at Meishan Section D (Fig. 13). Secondary markers for correlation include a magnetic reversal from normal to reverse within the C. wangi Zone as well as changes in fusulinid and ammonoid faunas. There are no major stable isotopic excursions coinciding with the boundary, but the lower Changhsingian is generally enriched with respect toδ13C values compared with the upper Wuchiapingian (Fig. 14).

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Fig. 13. The GSSP of the Wuchiapingian-Changhsingian boundary at the Meishan Section D (after

Jin et al., 2006).

Fig. 14. Integrated stratigraphic sequences around the Wuchiapingian-Changhsingian boundary in Meishan

Section D and the distribution of various fossil groups, carbon isotopes, geochronologic ages, and magnetic

reversals. Note that the lithologic succession is subdivided into both beds and units. The beds are based on

historical usage and are depicted to allow comparison with the literature. It isrecognized

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that these beds are actually bedsets or parasequences except in the case of the ash beds, which represent true

beds. The units are based on distinctive lithologic changes that reflect interpreted changes in depositional

environment (after Jin et al., 2006).

GSSP of the Permian-Triassic boundary at the Meishan Section D

The GSSP for the Permian-Triassic boundary was ratified by IUGS at Meishan Section D in 2001 (Yin et al., 2001). The boundary has been defined by the First Appearance Datum (FAD) of the conodont Hindeodus parvus, in the middle of Bed 27 (base of Bed 27c) of the lowest part of the Yinkeng Formation at Meishan Section D (Fig. 15). Secondary markers for the correlation include major carbon isotopic negative excursions from the top part of Bed 24e to Bed 25, immediately below Bed 27c, and the associated index fossils [ammonoid Ophiceras and bivalve Claraia wangi]. Additionally, the PTB stratigraphic sets including a limestone (Bed 12) bracketed by two ash beds (the “white clay”of Bed 25 and the “black clay”of Bed 26) around the PTB can be correlated in many PTB sections in South China (Fig. 15; Yin et al., 2001).

Fig. 15. The GSSP of the Permian-Triassicboundary at Meishan Section D (modifiedfromYin et al., 2001).

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Sedimentary features of the Permian-Triassic boundary sequence at the Meishan Section D (Zheng et al., 2013).

Bed 27 was usually considered comprising continuously-deposited, homogeneous silty limestone, with no depositional hiatus near the boundary. Detailed study on the boundary sequence revealed that a typical firmground characterized by Glossifungites ichnofacies developed about 2 cm below the Permian-Triassic boundary in Bed 27. Fossil content and lithology show apparent differences across the firmground crust. The abundance of the Permian bioclasts decreases significantly across the firmground, and is accompanied by a shift of dominating carbonate precipitation from calcite to dolomite. The firmground marked a rapid transgression at the very end of the Late Permian and significant shifts of sedimentary environment and paleoclimate.

This transgressive submerging surface is also observed at the Huangzhishan section of the shallow-water carbonate platform facies in Zhejiang Province, the Jiangya section of the lower-slope to basinal-margin facies in Hunan Province, the Pingdingshan section of the basinal facies in Anhui Province of South China, as well as the Selong section in Tibet of the northern peri-Gondwana. The transgressive submerging surface marks the onset of a rapid global transgression at the latest Permian.

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Day 2 (September 9th): Jiande-Guixi-Quzhou

Schedule:

08:00-11:30, Jiande to Guixi

11:30-12:00, [Stop 2-1: Downtown, Guixi county]. Investigating the Hekou Formation of

Guifeng Group, Upper Cretaceous

12:00-12:30, Lunch time

12:30-15:00, [Stop 2-2: Downtown and Yinshi-Jiangjia village, Guixi county]. Investigating

the Tangbian Formation of Guifeng Group, Upper Cretaceous

15:00-18:00, Guixi to Quzhou

18:20-, Dinner and accommodation in the Dijing Hotel, Quzhou City

Highlight: Large-scale aeolian facies, Tangbian Formation of Guifeng Group;

Intermountaine mollase facies, Hekou Formation of Guifeng Group (Upper Cretaceous)

Stop 2-1 Intermountaine mollase facies, Hekou Formation of Guifeng Group, Upper Cretaceous

Location: East of the downtown, Guixi county, Jiangxi province

Time: 30 minutes

Background:

In Xinfeng basin of Jiangxi Province, the Cretaceous is upward composed of the Huobashan Group, Ganzhou Group, and Guifeng Group (Fig.16). The Late Cretaceous Guifeng Group subsequently consists of the Hekou, Tangbian and Lianhe formations. The Hekou Formation is dominated by conglomerates, and was formed in the fluvial fan environment (Guo et al., 2013).The Tangbian Formation is characterized by reddish sandstones with two different sedimentary environments interpretation. Some people interpreted to be deposited in braided river and alluvial plain (Guo et al., 2013), while others interpreted to be the aeolian products (Jiang et al., 2008). The Lianhe Formation is composed of variable conglomerates, sandstone, siltstone, mudrocks, and it could be deposited in fluvial fan environment (Guo et al., 2013).

The chronostratigraphy of the Cretaceous Xinfeng basin is not well constrained due to lack of age-indicated fossils. The Huobashan Group is relatively better dated than other two groups as the zircon isotope dating indicate it is of Early Cretaceous (~144-132 Ma, Liu et al., 2009; 135-120 Ma, Li et al., unpublished ). The overlying Ganzhou Group and Guifeng Group are only roughly inferred to Late Cretaceous based on regional stratigraphic correlation and some plant fossils Onychiopsis, Coniopteris, Brachyphyllum, Elatocladus, Conites, Ginkgoites,

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Quercus, Sabalites, etc. ostrocod Cypridea, Cyprinotus, Candona, Ilyocpris, charophyte Grambastichara, Latochara, Gyrongona (e.g. Ling, 1996), pollen Classopollis, Exesipollenitea, Psophosphaera, etc. (Wu, 1992).

There are no fossils and mineral isotopes precisely indicating the age of the Hekou formation. Plant Manica sp. and other dinosaur egg fossils in Boyang may indicate it was deposited in the Late Cretaceous (Ling, 1996). Ling (1996) placed the (Hekou, Tangbian, Lianhe) three formations of the Guifeng Group as normally upward younger sequence, however, Xie (2001) suggested these three formations were likely formed in the same time, i.e. they are coevally superposed and deposited in different environments----comprising a deposystem composite of fluvial fan and river.

Fig. 16. Geological sketch of the Xinjiang Basin in eastern Jiangxi province (From Guo et al., 2013)

1-Quaternary; 2-Lianhe Formation; 3-Tangbian Formation; 4-Hekou Formation; 5-Zhoutian Formation; 6-Maodian

Formation; 7-Lower Cretaceous Huobashan Group; 8-Upper Jurassic Wuyi Group; 9-Pre-Cretaceous; 10-Granites;

11-Conformity; 12-Nonconformity; 13-Disconformity; 14-Fault

Observation:

The Hekou Formation is predominated by massive conglomerates with a few breccia. Most of conglomerates are round, subround, subangular with good, medium sorting. Parallel beddings are commonly associated with coarse sandstone, and trough cross-beddings occasionally occur. Some sieve sediments can be also found. Zhu et al. (2012) and Guo et al. (2013) interpreted the conglomerates had been formed in fluvial fan.

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Stop 2-2 Large-scale aeolian facies, Tangbian Formation of Guifeng Group, Upper Cretaceous

Location: Downtown and Yinshi village, Guixi county, Jiangxi province

Time: 2.5 hours

Background:

The Tangbian Formation is characterized by reddish sandstones with two different sedimentary environments interpretation. Some people interpreted to be deposited in braided river and alluvial plain (Guo et al., 2013), while others interpreted to be the aeolian products (Jiang et al., 2008).

Observation:

In the west (aside highway G320, near southern bus station) of downtown of Guixi, large-scale aeolian sandstones of the Tangbian Formation are well outcropped at lots of quarries. Large cross-beddings can be observed, and the set of cross-bedding is astonishingly up to ca. 20 m thick (Fig. 17). Sandstones are of purple-red, well-sorted, and round-grained (SEM images); medium to fine-grained with little suspension load. They have high-dip tabular planar characterized by aeolian dune foresets, wind-ripple lamination, typical aeolian grain surface textures such as dish-shaped impact scars, crescent-shaped impact scars (SEM images) and frosted surfaces (Jiang et al., 2008). At the point, paleo-current of wind was directed southward and eastward. In Xinjiang basin, the paleo-current reconstruction proved that the dominant prevailing winds were westerlies and the secondary prevailing winds were northeasterlies with a small amount of south-southeasterlies and north-northwesterlies (Jiang et al., 2008).

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Fig. 17. Photograph showing the large aeolian sandstone of the Tangbian Formation, town of Guixi

At Yinshi-Jiangjia village (N28°19′54.5″, E117°12′23.6″), ca. 15 km north to the former observation point along the countryside road X323, large aeolian sand dunes are easily accessed to observe, aiming to see surface and inner structures of cross-bedding set and wind-ripple lamination. On the surface of cross-bedding set, wavy wind-erosional surface, centimeter-decimeter order mudcracks are abundant (Fig. 18). Within the lamination, weathered/hydrocarbon bleaching caves are common. Some zibars (Zibar, a low-relief, rounded, coarse-grained, sand dune with no slipfaces. Regularly spaced zibars produce an undulating surface on otherwise level ground. Cited from the Dictionary of Earth Sciences (Ailsa Allaby and Michael Allaby, 1999). ) can be also observed. The ripples indicate a northeast wind-direction. At this point, it may also take half an hour. Near the village, lots of buildings (esp. ‘house’) constructed by red aeolian sandstones can be seen.

If we have time, we may drive to see paleosol near the first point. At the milestone marked as ca. 8.1 km of the Guibai route (X329), Wangchanghua village of Luohe town, several calcisol successions are developed in the middle Luotang/Zhoucun Formation of the Ganzhou Group. Within the calcisols, 5-10 cm size ginger-like calcretes are dense with up to 30-50% in content (Fig. 19). The carbon isotope of calcrete are 5.94-6.68‰, indicating ca. 1000-1300 ppmV of paleoatmospheric CO2 concentration in the late Albian (Li et al., 2014), over four times of human pre-industrialization level.

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Fig. 18. Photograph showing mudcrack on the aeolian cross-bedding set f the Tangbian Formation, Yinshi village,

north of Guixi

Fig. 19. Photograph showing dense calcretes of calcisol of the Luotang/Zhoucun Formation, Wangchanghua

village, southwest of Guixi

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Day 3(September 10th):Quzhou-Longyou-Jiande-Shipu

Schedule:

08:00-8:30, Quzhou to Longyou

8:30-9:30, [Stop3-1: West of Tashi Middle School, Longyou county]. Investigating the

Jinhua Formation of Quzhou Group, Upper Cretaceous

9:30-10:30, Longyou to Jiande

10:30-12:00, [Stop3-2: Tongjia, Zhoucun, and Yanxia of Shouchang town, Jiande

county]. Investigating the Jiande Group, Lower Cretaceous

12:00-13:00, Lunch at Shouchang Village

13:00-17:30, Jiande to Shipu

18:20-, Dinner and accommodation in the Sunmarina Hotel, Shipu village, Xiangshan county, Zhejiang Province

Highlight: Lacustrine facies, Jinhua Formation of Quzhou Group (Upper Cretaceous);

volcanic-sedimentary successions and paleosol facies of the Lower Cretaceous Jiande

Group.

Stop 3-1 Lacustrine facies, Jinhua Formation of Quzhou Group, Upper Cretaceous

Location: West of Tashi Middle School, ca. 12 km north to Longyou county, western Zhejiang

Time: half to one hour

Background:

Three Cretaceous continental basins were developed in western Zhejiang province including the Jiande Basin, the Yongkang Basin, and the Jinhua-Quzhou Basin. New studies on zircon chronology of volcanic intercalations indicate that the Yongkang Basin could be coevally formed with the Jiande Basin, while the Jinhua-Quzhou Basin was developed later (Fig. 20).

In Jinhua-Quzhou Basin, the Qujiang Group comprises upward the Zhongdai Formation, Jinhua/Lanxi Formation, and Quxian Formation (Fig. 20). The Zhongdai Formation is dated from the middle to upper Albian based on its relationship to the strata above and below, and K-Ar isotope dating (105 Ma) of basalt bulk in its lower part (ZBGM, 1996). Some fossils of plants, bivalves, and dinosaurs were found. The mid-lower part of the formation is composed of conglomerates, while sandstones and mudrocks with calcretes dominated in the upper part. The Jinhua Formation consists of sandstones and mudrocks, and the overlying Quxian Formation is composed of brownish red sandstones with conglomerates. These two latter formations are dated later than the Albian based on continetal fossil correlation (Yu and Xu, 1999).

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It is difficult to date the strata due to the same problem of terrestrial succession that are short of age- meaningful fossils. The Qujiang Group, including its subdivision formations, was roughly dated as the Late Cretaceous by the relation to the underlied and disconform- able volcanic Moshishan Group and some terrestrial fossils such as. Bivalves Sphaerium, Trigoniodes; ostracods Cristocypridea, concho- stracans Candoniella, Cypridea, Tenuestheria, Zhestheria; insects Siculicorixa, Plants Frenelopsis, Pseudofrenelopsis, and dinosur Chilantai- surus zhejiangensis.

Observation:

At the visiting site, ca. 100 m new outcrop of the Jinhua Formation (the third-fourth member of former Jinhua Formation) outcrops aside ponds by digging. Grayish purple and red silty mudrock and siltstone are the main lithologies. Horizontal lamination can be observed. Con- volute structures are developed between mudrocks and siltsto- nes/fine sandstones, indicating compacted dehydroration. The fine rocks with horizontal lamination suggest it could be accumulated in a lake environment.

Stop 3-2 Volcanic-sedimentary successions and paleosol facies of the Lower Cretaceous Jiande Group

Topic: Volcanic-sedimentary successions and paleosol facies of the Lower Cretaceous Jiande Group.

Location: Tongjia, Zhoucun, and Yanxia of Shouchang town, Jiande county, western Zhejiang

Fig. 20. Age data of isotopes and new stratigraphic framwork of the

Cretaeous basins in western Zhejiang province (Li et al., in

preparation)

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Time: 2-3 hours

Background:

In Jiande basin, the Jiande Group consist of four formations upward including the Laocun, Huangjian, Shouchang, and Hengshan formations (e.g. ZBGM, 1996; Chen, 2000). The sequence and relationship of these formations were revised in the Figure 16 based on zircon chronology of volcanic intercalations (Li et al., 2011).

The Laocun Formation is composed of dark-purple muddy siltstones, sandstones and mudrocks interbedded with tuff and rhyolite with some fossils of gastropods, ostracods, insects, and plants (e.g., Cladophlebis sp.). The lower part is dominated by conglomerates nonconformiblely overlying on the marine Upper Paleozoic sequence (Fig. 21). This formation was dated as the Hauterivian-Barremian age by zircon U-Pb isotope dating (Li et al., 2011). The volcanic rocks of the Huangjian Formation was dated in the Aptian age. The Shouchang Formation are variegated tuffaceous sandstones and shales with two layers of volcanic rocks in the middle and upper part. Some fossils of fishes, insects, gastropods, bivalves, conchostracans, and plants were reported within this stratum (e.g. Jiang et al., 1993; ZBGM, 1996; Chen, 2000). The Hengshan Formation is dominated by reddish-purple muddy siltstones and silty mudrocks with sandstones and volcanic intercalations, within which fossils of gastropods, bivalves and plants (e.g. Conioperis sp.) were found (e.g. Jiang et al., 1993; ZBGM, 1996; Chen, 2000). The Shouchang and Hengshan formations are early to middle Aptian in age based on zircon U-Pb chronlogy (Li et al., 2011). Calcretes were sampled within mudrock of the Hengshan Fm for C-O isotope analysis, indicating possible calcisols.

Observation:

Here we will mainly examine the succession of volcanic-sedimentary rocks at observation site (1) and site (2), and see the calcisol at site (3) (Fig. 21).

——At the observation site (1), pyroclastic rocks of the volcanic-sedimentary Laocun Formation are well exposed at a quarry near Hucun and Hucunxi villages. Greenish massive crystal tuff, tuffites, breccia are the main lithologies, in which zircon U-Pb isotopes of the tuff yielded an age of 130.0±3.3 Ma (sample 128-04ZK, Li et al., 2011), indicating the Hauterivian in age. Other samples near the site show ages of zircon U-Pb isotopes range ca. 138-125 Ma (Fig. 22), the interval of the Vanlangian-Barremian for the Laocun Formation (Li et al., 2011).

In the sedimentary succession of the Laocun Formation, some fossils of gastropods Amplovalvata, insects Linicorixa, Lycoriomima, Mesopanorpa,Tinactum, ostracods Rhinocypris, plants Cladophlebis, etc. were reported (Jiang et al., 1993; ZBGM, 1996; Chen, 2000).

On the way to Zhoucun, the next stop, gray medium-thick sandstones and laminated (algal) mat siltstone-shale can be seen in the middle part of the Laocun Formation aside the road. Parallel bedding, and planar-trough cross-bedding in sandstones may indicate a meandering environment, and laminated (algal) mat siltstone-shale could be accumulated in lake.

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Fig. 21. Geological sketch of Shouchang area, Jiande, Zhejiang (from Jiang et al., 1993) showing the localities of

observation points and sections at stop 3-2

1-Upper Paleozoic; 2-Laocun Formation; 3-Huangjian Formation; 4-Lower Member of Shouchang Formation;

5-Middle Member of Shouchang Formation; 6-Upper Member of Shouchang Formation; 7-Hengshan Formation;

8-Quaternary; 9-unconformity; 10-fault; 11-inferred fault of this work; 12-locality of the section; 13-observation

point; 14-river; 15-village and town; 16-freeway

————At the observation site (2), the Huangjian and Shouchang Formations will be observed.

Starting at Zhoucun village, reddish pyroclastic rocks and tuffaceous mudrock-siltstones of the Huangjian Formation expose in about 200 m thick along the road. The chronology of the zircon U-Pb isotope indicates it could be separated by a fault (Fig. 22). Namely the stratum is composed of two parts: the lower part was continuously deposited on the Laocun Formation, and the upper part was coeval with the Laocun Formation (Fig. 20 and 22). In this section, no fossils was ever reported.

Above the Huangjian Formation, the Shouchang Formation becomes dark gray, and it is bounded by two series of pyroclastic rocks. The absolute ages of the zircon U-Pb isotopes from the pyroclastic rocks are 127.1±1.1 Ma and 123.8±1.0 Ma, respectively, indicating the formation was formed in the Barremian-early Aptian. The middle part of the Shouchang Formation is characterized by dark gray, greenish gray (silty, calcareous, tuffaceous) shales, tuffaceous siltstones which probably was deposited in lake environment. Lots of fossils have been found in shales, including gastropods Probaicalia, Viviparus; Bivalves Ferganoconcha, Mengyinaia; ostracods Damonella, Darwinula; conchostracans Yanjiestheria; insects Clypostemma, Ephemeropsis; fishes Fuchunkiangia, Ganaid, Mesoclupea, Sinamia, and plants Klukia (e.g. Jiang et al., 1993; ZBGM, 1996; Chen, 2000). The fossil association may indicate a late mid-Cretaceous in age.

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Fig. 22. Profile of the Zhoucun-Yanxia cross section with zircon age sample horizons in north of Shouchang town,

Jiande county, Zhejiang province (Original cross section after Ding et al., 1989)

————At the observation site (3), the paleosol succession will be examined.

The upper Hengshan Formation is newly outcropping along a path of high-voltage wire system near Shanggui and Xiagui villages (N29°22′56.2″, E119°12′32.6 ″). It dips eastward in the normal sequence. There are at least seven paleosol cycles occurring in the upper part of the formation. An individual paleosol is featured by calcisol, i.e. pedogenic calcretes are the remarkable composition within the BK (subsurface horizon enriched pedogenic carbonates below surface horizon of the mixed organic and clay material). Calcretes are mostly 1-3 cm in size and 0.5-2% in content, dark purple, grayish purple BKs are 0.4-1.8 m thick (Fig. 23). A single calcisol cycle ranges 6-12 m in thickness, which was developed in lithofacies of either alluvial plain, or overbank, or interchannel. By ~120 Ma of zircon isotope from pyroclastic intercalation, the upper part of the Hengshan Formation was assigned an age of late Aptian (Fig. 20). The calcisols indicate a arid-semiarid climate during the late Aptian in the Jiande Basin.

In the Jiande basin and adjacent regions, fossils have been found and described including gastropods Lioplacodes, Mesoneritina, Probaicalia, Viviparus; Bivalves Nakamuranaia; and plants Cladophlebis, Coniopteris, Frenelopsis, Otozamites (e.g. Jiang et al., 1993; ZBGM, 1996).

Besides of the Hengshan Formation, calcisols also occur in the Laocun and Huangjian formations, indicating arid-semiarid climate was alternated with semi-humid climate (e.g. dark lacustrine facies in the middle part of the Shouchang Formation) during Early Cretaceous in Jiande Basin. This climate scenario is consistent with that in South China during the same period. For excample, pCO2 estimates from the carbon isotope of the Early Cretaceous calcretes are 1000-2000 ppmV (Li et al., 2014), implying a possible hot climate in the this region.

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Fig. 23. Photograph showing calcretes within the second calcisol BK from the upper Hengshan Formation,

Shouchang, Zhejiang province

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Day 4 (September 11th): Shipu-Nanjing

Schedule:

9:00-10:40, [Stop 4-1: Shipu village, Xiangshan county]. Investigating the Shipu Group,

Lower Cretaceous

10:40-11:40, Lunch at Shipu

11:40-18:40, Shipu to Nanjing

Highlight: Transitional facies, Shipu Group, Lower Cretaceous

Stop 4-1 Transitional facies, Shipu Group, Lower Cretaceous

Location: Shipu village, Xiangshan county, Zhejiang Province

Time: 2-3 hours

Background:

In the Shipu village of Zhejiang Province, coastal southeastern China, the Shipu section is a unique, relatively complete and well-exposed Lower Cretaceous limestone-bearing section within the late Mesozoic active volcanic belt. In addition to the limestones, the rocks of the succession include silicified tuffaceous sandstone, silicified mudstones, and several tuff interbeds (Zhejiang Geology and Mineral Resources Bureau, 1996) (Fig. 24).

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Fig. 24. Schematic map showing the location of the “Shipu limestones” section in eastern Zhejiang Province(Hu et

al., 2012b)

From the Middle Triassic to the Early Jurassic, most of southeast China was initially folded and uplifted, and then subjected to extension and collapse in response to the Indosinian orogeny. Hence, the Middle Triassic is absent from most areas. The residual Upper Triassic–Lower Jurassic consists of conglomerates and coarse-grained sandstones, feldspar sandstones, quartz sandstones and siltstones with carbonaceous mudstones and coal bed intercalations. Marine deposits have a restricted and local distribution such as in southern Guangdong Province (Hu et al., 2012a).

Since the Yanshanian period, volcanism and magmatism have dominated in southeastern China, being stimulated by the westward subduction of the Palaeo-Pacific plate under the Eurasian continental margin (Gilder, 1996; Li, 2000; Wang and Zhou, 2002). The depositional environment is widely believed to have changed from marine to continental. The Middle Jurassic is mainly composed of terrestrial clastic rocks and bimodal volcanic rocks, while the Upper Jurassic is absent according to recent mapping results of the area at 1:250,000 and 1:50,000 scales.

From the Early Cretaceous, the area experienced two basin-building stages. The first of these occurred at approximately 145–100 Ma (Early Cretaceous) and is characterized by volcanic faulted-depressions (Jahn, 1974; Jahn et al., 1990; Zhou et al., 2006). The second occurred at approximately 100–70 Ma (Late Cretaceous

30

–Palaeogene) and is characterized by red-coloured sedimentary rocks. Corresponding to this two-stage basin development, the Lower Cretaceous is mainly composed of rhyolite and welded and crystalline-clastic tuffs. The Upper Cretaceous consists mainly of red siltstones, mudstones and intercalated basalts (Hu et al., 2012a).

The Palaeogene comprises mostly grey to purple coarse-grained fragmentary rocks, siltstones, mudstones and intercalated gypsum and oil-bearing shales. The Neogene consists of brown to yellow siltstones and is present locally (Hu et al., 2012a).

To summarize, coastal southeast China was uplifted and became a continental region after the Indosinian orogeny. Widespread tectonic expansion and a volcanic-sedimentary succession developed during the subsequent Yanshanian period. Marine limestones commonly developed between the Devonian and the Permian. Hence, the Shipu limestone-bearing section in the late Mesozoic volcanic belt is important for determining the depositional environment and tectonic background of the late Mesozoic volcanism (Hu et al., 2012a).

Observation:

(1) Strata from the Shipu section

The base of the section has faulted contacts with the volcanic breccia and ignimbrite of the Lower Cretaceous Moshishan Group, and the top is in contact with an intrusive vein, which is covered by Quaternary sediments. As shown in Fig. 21, the lower part of the section (0–30 m) consists mainly of volcanic breccia interbedded with tuffaceous sandstones. In contrast, the upper part (30–120 m) consists mainly of silicified tuffaceous sandstones and siltstones, silicified mudstone and shales, and limestones. Approximately three deepening-upward cycles can be recognized. Each of these begins mainly with tuffaceous sandstones or siltstones and ends with limestones interbedded with mudstones and shales (Hu et al., 2012a; Fig. 25).

Fig. 25. Sketh of the Shipu scetion located in Xiangshan of Zhejiang Province (Wang et al., 2012)

(2) Lithofacies of the Shipu Group

As mentioned above, the limestones in the section are the key for interpretation of 31

sedimentary environment. The limestones in the section are mainly stromatolite algal-bonded, oolitic, bioclastic, and micritic limestones and marl. Three limestone units are separated by tuffaceous clastic beds (Fig. 26). All three yield representative marine fossils, such as Sinoditrupa conica, Acerrotrupa aggregata, Spirorbis (Dexiospira) jiangsuensis, Coccolithophyceae and Rhaphoneis cf. surirella, indicating a marine origin for the limestones (Hu et al., 2012a).

Fig. 26. Photographs showing outcrop sections and the deposited rocks (Hu et al., 2012a)

Stromatolites

Stromatolites are well developed and are usually associated with conglomerates, sandstones and siltstones (Figs. 27a, b). The stromatolites are 5 cm to 0.5 m in height, and 20 cm to 2 m in diameter. The growth laminae are mm to cm thick. Columnar and domal stromatolites are the most commonly observed types of stromatolites. In addition, plate-like stromatolites are also found. The stromatolites are believed to be formed in an intertidal to subtidal environment (Hu et al., 2012a).

Algal boundstone

The algal boundstones occur as laminar beds intercalated within the irregular horizontal mudstones and siltstones. Shrinkage cracks of surface mats due to evaporation demonstrate that the depositional environment varied from muddy intertidal to supratidal. The black alga layers alternate with the grey boundstone layers. Volcanogenic and carbonate detritus present in the black algal layers are observed along the bedding (Fig. 27c). In addition, the sand shadow structures associated with stromatolites are observed on certain sandy bed surfaces. They are indicatives of a supratidal to shallow subtidal marine environment (Hu et al., 2012a).

Oolitic limestone

The oolitic limestones are mainly oosparites. The proportion of matrix is less than 15%. Approximately 90% of the ooids with volcanogenic detrital nuclei are crusted with sparry calcites (Fig. 27d). The diameter of the ooids ranges between 250 µm and 500 µm (Hu et al., 2012a).

Bioclastic limestone 32

The bioclastic limestones with marine bioclastic detritus, such as ostracode and brachiopod shells, are mainly grey massive biomicrites. The matrix is micrite with a relative abundance of approximately 50% (Fig. 27e).

Micritic limestone

The micrite limestones are gray and either are massive or have laminar horizontal beds (Fig. 27f). The abundance of the micrite matrix is greater than 90%. This high matrix level reflects a low-energy water environment, such as the upper part of intertidal flat or below the storm wave base level (Hu et al., 2012a).

Fig. 27. Limestones in the Shipu section (Hu et al., 2012a)

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