Julien Morin

Marc Jolivet

Cécile Robin

Gloria Heilbronn

Laurie Barrier

Sylvie Bourquin

Yingying Jia

JURASSIC PALEOGEOGRAPHY OF THE TIAN SHAN: AN EVOLUTION DRIVEN BY FAR-FIELD TECTONICS AND CLIMATE

The strongly intracontinental Tian Shan region, in Central Asia represents a key area to understand the long term evolution of continents in general and Asia in particular. If its Paleozoic and Cenozoic geodynamics are well understood, its Mesozoic evolution remains poorly constrained. In order to decipher the paleogeographic and large-scale tectonic evolution of the Tian Shan area during the Jurassic, we compiled, detailed field analyses of sedimentary rocks acquired within and around the Chinese Tian Shan region together with previously published data. We present three paleogeographical maps corresponding to the late Earlyearly Middle Jurassic, late Middleearly Late Jurassic and Late Jurassic -Early Cretaceous transition periods. We provide a large -scale picture of the Jurassic paleogeographic and climatic evolution of the Tian Shan region and discuss the geological

the Late Jurassic is also recorded in the sedimentary series all over the region. At that time, few evidences of deformation exists in the Tian Shan or within the Caspian -Turan domains.

We propose that the late Middleearly Late Jurassic corresponded to a period of relative tectonic quiescence in the area. Finally, the Late Jurassic -Early Cretaceous transition was marked by a tectonic reactivation leading to the inversion of the Yarkand -Fergana Basin and to localized relief building in the Tian Shan. This renewed transpressive deformation phase could be mainly related to the coeval accretion of the Helmand block to the south-west, and possibly to the onset of the accretion of the Lhasa Block along the southwestern margin of Eurasia. Finally, this period was also characterized by the climax of aridification which played a major role on the emplacement of extensive alluvial fan systems in the basins surrounding the range.

KEYWORDS: Jurassic, Tian Shan, Paleogeography, Climate, Tectonics

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INTRODUCTION

The long-term geodynamic evolution of Asia is characterized by a succession of orogenesis driven by accretion of continental blocks along the southern margin of the continent (e.g., [START_REF] Jolivet | Mesozoic tectonic and topographic evolution of Central Asia and Tibet: a preliminary synthesis[END_REF]. These collisional orogenic events succeeded one another from the Paleozoic, with the final accretion of the Central Asian Orogenic Belt during the Permian (e.g., [START_REF] Windley | Tectonic models for the accretion of the Central Asion Orogenic Belt[END_REF][START_REF] Wilhem | The Altaids of Central Asia: a tectonic and evolutionary innovative review[END_REF], the Permian-Triassic Indosinian orogeny and the closure of the paleo-Tethys ocean (e.g., [START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF][START_REF] Roger | Late Paleozoic to Jurassic tectonic evolution of the Bogda area (northwest China): Evidence from detrital zircon U-Pb geochronology[END_REF], the Mesozoic accretion of the various blocs that form the Tibetan and South Caspian domains (e.g., Zonenshain and Le Pichon 1986;[START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF][START_REF] Brunet | The South Caspian Basin: a review of its evolution from subsidence modelling[END_REF], the Cretaceous closure of the Mongol-Okhotsk ocean in Siberia (e.g., [START_REF] Enkin | The paleomagnetic record of uppermost Permian, Lower Triassic rocks from the south China block[END_REF][START_REF] Zorin | Geodynamics of the western part of the Mongolia-Okhotsk collisional belt, Trans-Baikal region (Russia) and Mongolia[END_REF]Cogn Jolivet et al., 2017b), and finally the Cenozoic collision of India (e.g., [START_REF] Tapponnier | Oblique stepwise rise and growth of the Tibet Plateau[END_REF]. These successive events bring the idea of a continent essentially affected by compressive deformation and largely characterized by the growth of large mountain ranges. Within this largely compressive geodynamic setting, the Jurassic period corresponds to a peculiar time span comprised between two major orogenic events: 1) the Cimmerian orogeny which began during the late Paleozoic and ended during the Triassic -Jurassic transition (e.g., Sengör, 1979;[START_REF] Watson | Plate tectonic history, basin development and petroleum source rock deposition onshore China[END_REF]Mattauer et al.1992;[START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF][START_REF] Metcalfe | Gondwana dispersion and Asian accretion: tectonic and palaeogeographic evolution of eastern Tethys[END_REF] and 2) the Cenozoic Himalayan orogeny (e.g., Molnar and Taponnier, 1975;Yin, 2009). During the Jurassic, the Eurasian continent was mostly surrounded by subduction zones leading to late Early -Middle Jurassic extension within the Caspian -Turan domains (e.g., Zonenshain and Le Pichon 1986;Nikishin et al. 1998;[START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF][START_REF] Brunet | The South Caspian Basin: a review of its evolution from subsidence modelling[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF][START_REF] Robert | Structural evolution of the Kopeh Dagh fold-and-thrust belt (NE Iran) and interactions with the South Caspian Sea Basin and Amu Darya Basin[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF] and to Late Jurassic -Cretaceous extension within the Siberian -Mongolian domains (e.g., [START_REF] Zorin | Geodynamics of the western part of the Mongolia-Okhotsk collisional belt, Trans-Baikal region (Russia) and Mongolia[END_REF]Graham et al., 2001;[START_REF] Johnson | Polyphase evolution of the East Gobi basin: sedimentary and structural records of Mesozoic-Cenozoic intraplate deformation in Mongolia[END_REF][START_REF] Daoudene | The Ereendavaa Range (north-eastern Mongolia): an additional argument for Mesozoic extension throughout eastern Asia[END_REF][START_REF] Donskaya | Age and evolution of late Mesozoic metamorphic core complexes in southern Siberia and northern Mongolia[END_REF][START_REF] Ritts | Early Cretaceous supradetachment basins in the Hohhot metamorphic core complex, Inner Mongolia, China[END_REF]). However, the Jurassic paleogeographic and kinematic evolution of the probable relay

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zone corresponding to the Tian Shan region in Central Asia is yet to be fully understood.

Some studies indicate that during its Jurassic evolution, this area was dominated by progressive planation of the Tian Shan relief [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF] while others propose that the region underwent recurrent periods of relief building (e.g., Allen et al., 1991;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. Recurrent tectonic activity did occur during that period but the kinematics and driving mechanisms of these events are highly debated.

Some consider that the Tian Shan region was dominated by strike-slip and transtensive tectonics in a rather quiescent geodynamic setting (Jolivet et al., 2013) whereas others propose that the Tian Shan was rather under a compressional setting related to far-field collisions (e.g., [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Greene | Sedimentary record of Mesozoic deformation and inception of the Turpan-Hami basin, northwest China[END_REF][START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF][START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF].

Finally, a Late Jurassic -Early Cretaceous tectonic reactivation has been recorded by low-temperature thermochronology data within the Kyrgyz Tian Shan, although to the east, in the Chinese Tian Shan, the same type of data only suggest slow cooling [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF][START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2012, 2013;[START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. At the same period, extensive alluvial fan systems have been deposited in several basins surrounding the Tian Shan Range. These alluvial fans were inferred to have been formed in response to renewed tectonic activity [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. Moreover, a rapid transition from humid conditions that prevailed during the Middle Triassic to Middle Jurassic to a semiarid/arid climate that developed during the Late Jurassic -Early Cretaceous period also occurred in the Tian Shan area [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF]Shao et al., 2003;Jolivet et al., 2017a). This change in climatic conditions is thought to have had a major impact on the paleogeographical evolution of this region by controlling the emplacement of the extensive Late Jurassic -Early Cretaceous alluvial fan systems (Jolivet et al., 2017a).

However, available descriptions of the Jurassic paleogeography or tectonic evolution of the

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5 Tian Shan Range usually address too restricted areas and/or stratigraphic intervals to fully understand the impact of far-field deformation within this peculiar period in Central Asia history (e.g., Shao et al., 2003;[START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Feng | Sequence stratigraphy, sedimentary systems and petroleum plays in a low-accommodation basin: Middle to upper members of the Lower Jurassic Sangonghe Formation, Central Junggar Basin, Northwestern China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]Jolivet et al., 2017a;[START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF].

Therefore, in order to better understand the paleogeographic and large-scale tectonic evolution of the Tian Shan area, we compiled, our own detailed field analyses of sedimentary rocks in various basins associated with the range and previously published data to construct three paleogeographic maps for the periods of to the late Earlyearly Middle Jurassic, late Middle-early Late Jurassic and Late Jurassic -Early Cretaceous transition. We provide a large -scale picture of the Jurassic paleogeographic and climatic evolution of the Tian Shan region and discuss the kinematic evolution of the range together with the possible driving mechanisms.

GEOLOGICAL SETTING

1. LATE PALEOZOIC LITHOSPHERIC STRUCTURES AND MESO-CENOZOIC

REACTIVATIONS:

The lithospheric structure of the Tian Shan results from the late Paleozoic amalgamation of continental blocks and magmatic arcs along the southern margin of the Central Asian Orogenic Belt (CAOB; Sengör et al., 1993;[START_REF] Windley | Tectonic models for the accretion of the Central Asion Orogenic Belt[END_REF][START_REF] Charvet | Palaeozoic tectonic evolution of the Tianshan belt[END_REF]Alexeiev et al., 2017b). Subsequently, the Tian Shan Range underwent transpressive deformation during the Permian -Early Triassic in response to the oblique convergence between Siberia and Baltica [START_REF] Bazhenov | Permian paleomagnetism of the Tien Shan fold belt, Central Asia: post-collisional rotations and deformation[END_REF][START_REF] Van Der Voo | Late orogenic, large-scale rotations in the Tien Shan and adjacent mobile belts in Kyrgyzstan and Kazakhstan[END_REF]. This induced dispersed rotations and motion along numerous strike-slip faults such as the Talas -Fergana fault, the Nikolaev line or the North Tian Shan fault (Fig. 1) (e.g., Allen et al., 1991; Laurent-

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6 Charvet et al., 2002;[START_REF] Buslov | Late paleozoic-early Mesozoic geodynamics of Central Asia[END_REF]Van der Voo et al., 2006 and references therein;Rolland et al., 2013). An alternative model proposed that counterclockwise rotation of the Yili -West Junggar blocks with respect to Tarim and Siberia induced large strike-strike slip motions along the previously mentioned lithospheric faults, resulting in about 1160 ± 380 km lateral displacement in the Tian Shan belt (Wang et al., 2007a). Independently to the tectonic model, thermochronology data recorded a strong Permian-Triassic cooling-exhumation phase within the Tian Shan Range implying the build-up of a major topography during that period [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF].

During the Meso-Cenozoic, the Paleozoic faults played a major role in localizing the deformation during the successive tectonic episodes that affected the Tian Shan Range (Allen et al., 1991[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Sobel et al., 1999;[START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]Rolland et al., 2013;Alexeiev et al., 2017). From the Triassic to the Cretaceous, several accretion-collision events (generally known as the Cimmerian Orogeny) took place along the southern Eurasian margin including the collision of the Qiangtang (Late Triassic-Early Jurassic), Lhasa (Late Jurassic-Early Cretaceous) and the Kohistan-Ladakh (Late Cretaceous) blocks [START_REF] Matte | Tectonics of Western Tibet, between the Tarim and the Indus[END_REF][START_REF] Kapp | Geological records of the Lhasa-Qiangtang and Indo-Asian collisions in the Nima area of central Tibet[END_REF][START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF]. These events induced the reactivation of the Palaeozoic structures, which led to crustal deformation in the Tian Shan area [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF]. Finally, tectonic reactivation related to farfield effects of the India-Asia collision initiated during the late Oligocene -Miocene and led to the growth of the present-day Tian Shan Range (e.g., Molnar and Taponnier, 1975;[START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF]Sobel et al., 1999;[START_REF] Macaulay | Cenozoic deformation and exhumation history of the Central Kyrgyz Tien Shan[END_REF][START_REF] Jia | Cenozoic tectono-geomorphological growth of the SW Chinese Tian Shan: Insight from AFT and detrital zircon U-Pb data[END_REF].

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LATE PALEOZOIC -EARLY CRETACEOUS EVOLUTION OF THE TIAN SHAN SEDIMENTARY BASINS

1. The Junggar Basin

The Junggar (Fig. 1) is an intracontinental basin bordered by the Tian Shan Range to the south, the Halaalate mountains to the west, and the Altai Range to the north-east. This basin preserves, in its thickest part, around 16 km of late Paleozoic to Quaternary sediments.

The formation of the Junggar Basin followed the southward subduction of the North Tian Shan Ocean underneath the Yili block and its subsequent Late Carboniferous -Early Permian closure (e.g., [START_REF] Gao | Paleozoic tectonic evolution of the Tianshan orogen, northwestern China[END_REF][START_REF] Wang | Late Paleozoic tectonic evolution of the northern West Tian Shan, NW China[END_REF][START_REF] Charvet | Palaeozoic tectonic evolution of the Tianshan belt[END_REF]. Depending on the authors, the Junggar Basin initiated either during the Late Carboniferous in a post-collisional extensional setting [START_REF] Qiu | Tectono-thermal evolution of the Junggar Basin, NW China: constraints from Ro and apatite fission track modelling[END_REF][START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF][START_REF] Liu | Lahar facies of the latest Paleozoic Arbasay Formation: Geomorphological characters and paleoenvironment reconstruction of Northern Tian Shan, NW China[END_REF] or during the Permian as a response to a transtensional tectonics (Allen et al., 1991) associated with magmatism (Carrol et al., 1995;[START_REF] Wang | Evolution of calc-alkaline to alkaline magmatism through Carboniferous convergence to Permian transcurrent tectonics, western Chinese Tianshan[END_REF].

In this basin, the Upper Carboniferous strata consist of interbedded marine mudstone, siltstone and rare clayey limestone units followed upward by thick units of sandstone [START_REF] Novikov | Reconstructing the stages of orogeny around the Junggar basin from the lithostratigraphy of Late Paleozoic, Mesozoic, and Cenozoic sediments[END_REF]. The Lower Permian then marks the end of marine sedimentation with the deposition of a regressive sequence representing the final retreat of the sea from the South Junggar and the onset of continental sedimentation [START_REF] Carroll | Junggar basin, northwest China: trapped Late Paleozoic ocean[END_REF][START_REF] Carroll | Late Paleozoic tectonic amalgamation of northwestern China: sedimentary record of the northern Tarim, northwestern Turpan, and southern Junggar basins[END_REF]. The top of the Permian sequence consists of conglomerates, sandstones, siltstones and mudstones interpreted as alluvial plain and lacustrine deposits [START_REF] Carroll | Late Paleozoic tectonic amalgamation of northwestern China: sedimentary record of the northern Tarim, northwestern Turpan, and southern Junggar basins[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF].

During the Triassic, the Junggar Basin evolved either as a foreland basin [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF] or as a transtensional basin (Allen et al., 1995). Lower and Middle

Triassic units consist of conglomerates, sandstones and red to brown siltstones typical of

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continental sediments deposited in alluvial fan and alluvial plain environments. They are locally associated to caliche beds indicating deposition in seasonal semi-arid to arid conditions [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF]Nivokov, 2013). Finally, the Upper Triassic sedimentary rocks consist of interbedded conglomerates, sandstones and grey siltstones interpreted as deposited in alluvial fan to alluvial plain environments under humid conditions [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Ashraf et al., 2010;[START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF]Nivokov, 2013).

Subsequently, the Junggar Basin is thought to have evolved either as a flexural depression [START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Lin | Distribution and erosion of the Paleozoic tectonic unconformities in the Tarim Basin, Northwest China: significance for the evolution of paleo-uplifts and tectonic geography during deformation[END_REF][START_REF] Feng | Sequence stratigraphy, sedimentary systems and petroleum plays in a low-accommodation basin: Middle to upper members of the Lower Jurassic Sangonghe Formation, Central Junggar Basin, Northwestern China[END_REF] or as a transpressional basin [START_REF] Dengfa | Development and genetic mechanism of Chepaizi-Mosuowan uplift in Junggar Basin, China[END_REF][START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF] during the Jurassic period. The contemporaneous conglomeratic to sandy and silty deposits are mainly related to alluvial to lacustrine environments [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Feng | Sequence stratigraphy, sedimentary systems and petroleum plays in a low-accommodation basin: Middle to upper members of the Lower Jurassic Sangonghe Formation, Central Junggar Basin, Northwestern China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. The occurrence of widespread coal deposits in the Lower to Middle Jurassic series suggests humid conditions (e.g., [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. Upper Jurassic series are then characterized by the disappearance of coal and by the formation of calcareous paleosols indicative of semi-arid conditions [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Jolivet et al., 2017a). Finally, the Jurassic-Cretaceous transition is characterized by the emplacement of well-developed conglomerates thought either to mark a tectonic reactivation of the Tian Shan Range [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF] or to be mostly driven by climate (Jolivet et al., 2017a).

The intra-mountain basins

Several intra-mountain basins such as the Yili, Bayanbulak, and Turfan basins are preserved within the interior of the Tian Shan Range (Fig. 1).They formed concurrently to the Junggar Basin and are associated to the same late Paleozoic post-orogenic phase of extensive

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or transtensive deformation [START_REF] Wang | Late Paleozoic tectonic evolution of the northern West Tian Shan, NW China[END_REF][START_REF] Wang | Evolution of calc-alkaline to alkaline magmatism through Carboniferous convergence to Permian transcurrent tectonics, western Chinese Tianshan[END_REF][START_REF] Charvet | Paleozoic structural and geodynamic evolution of eastern Tianshan (NW China): welding of the Tarim and Junggar plates[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF][START_REF] Xia | Reassessment of petrogenesis of Carboniferous-Early Permian rift-related volcanic rocks in the Chinese Tianshan and its neighboring areas[END_REF].

The Yili Basin is bordered by the Borohoro Range (North Tian Shan) to the north and by the Narat Range (South Tian Shan) to the south. In its thickest part, this basin preserves around 5 km of Permian to Quaternary sediments. Its Permian series consist of marine sediments followed by the emplacement of volcanics and volcanoclastics deposits during the Upper Permian [START_REF] Li | Dynamic processes from plate subduction to intracontinental deformation: Insights from the tectono-sedimentary evolution of the Zhaosu-Tekesi Depression in the southwestern Chinese Tianshan[END_REF]. These series are uncomformably overlaid by the Triassic sediments, implying tectonic deformation at least up to the Lower Triassic [START_REF] Li | Dynamic processes from plate subduction to intracontinental deformation: Insights from the tectono-sedimentary evolution of the Zhaosu-Tekesi Depression in the southwestern Chinese Tianshan[END_REF].

Jurassic series consist of alluvial, lacustrine delta and lake deposits containing extensive coal beds that indicate humid conditions [START_REF] Li | Geological controls on coal quality of the Yili Basin, Xinjiang Northwest China[END_REF]. However this basin does not contain Upper Jurassic -Lower Cretaceous sediments (AGMCA, 2008).

The Bayanbulak Basin is located between the Narat Range to the north, the South Tian Shan Range to the south, and the Erbin Shan Range to the east. It preserves Mesozoic and Cenozoic sediments but its late Paleozoic to Mesozoic evolution is poorly known.

The Turfan Basin is a flexural basin containing in its deepest part around 7 km of Permian to Quaternary sediments (Shao et al., 1999). It is located between the Bogda Shan-Barkhol Tagh ranges to the north and the Chöl Tagh mountain range to the south. Its Lower Permian strata consist of continental and marine deposits interbedded with volcanic and volcanoclastic series (Shao et al., 1999;[START_REF] Wartes | Permian sedimentary record of the Turpan-Hami basin and adjacent regions, northwest China: Constraints on postamalgamation tectonic evolution[END_REF]. During the Late Permian -Early Cretaceous, the Turfan Basin then evolved as a compressive basin [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Allen et al., 1993;Shao et al., 1999;[START_REF] Wartes | Permian sedimentary record of the Turpan-Hami basin and adjacent regions, northwest China: Constraints on postamalgamation tectonic evolution[END_REF]. Its Upper Permian to Early Cretaceous series are entirely continental and consist of alluvial to lacustrine deposits [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Shao et al., 1999;[START_REF] Greene | Sedimentary record of Mesozoic deformation and inception of the Turpan-Hami basin, northwest China[END_REF][START_REF] Wartes | Permian sedimentary record of the Turpan-Hami basin and adjacent regions, northwest China: Constraints on postamalgamation tectonic evolution[END_REF].

In the Kyrgyz Tian Shan, the Issyk-Kul, Naryn, Aksai and Ming-Kush basins are intramountain depressions containing Jurassic to Quaternary sediments (Fig. 1) [START_REF] Lasovskiy | collisional s ik -s ip d fo m ions in Ti nsh n nd y E s n Xinji n[END_REF][START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF][START_REF] Macaulay | Cenozoic deformation and exhumation history of the Central Kyrgyz Tien Shan[END_REF]; De Pelsmaeker et , 2018). In the Issyk-Kul Basin, these sedimentary rocks consist mainly of alluvial to shallow lacustrine deposits containing numerous coal beds and plant fragments indicating humid conditions but they also contain caliche -type paleosols more typical of semi-arid conditions [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. The Ming-Kush Basin is a narrow transpressive depression containing 100-680m thick Jurassic deposits resting unconformably on Paleozoic basement rocks [START_REF] Lasovskiy | collisional s ik -s ip d fo m ions in Ti nsh n nd y E s n Xinji n[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. They mainly consist of alluvial plain, fan delta and shallow lacustrine deposits associated with coal-rich layers and plant fragments indicating humid conditions [START_REF] Lasovskiy | collisional s ik -s ip d fo m ions in Ti nsh n nd y E s n Xinji n[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Finally, Jurassic sedimentary rocks consisting mainly of coalbearing continental deposits resting unconformably on Paleozoic rocks occur in both the Naryn and Aksai basins [START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]AGMCA, 2008).

A C C E P T E D M A N U S C R I P T 10 al.

3. The Tarim Basin

The Tarim Basin (Fig. 1) is a large intracontinental basin located between the Tian Shan to the north, and the Western Kunlun and Altyn Tagh ranges to the south. In its thickest part, it contains up to 16 km of Late Precambrian to Quaternary sediments. This basin underwent multiple phases of tectonic deformation since the Late Precambrian [START_REF] Desheng | Hydrocarbon accumulations in the Tarim basin, China[END_REF]. The Tarim craton accreted to the Kazakhstan-Yili terrane in the Late Carboniferous-Early Permian during the final amalgamation of the CAOB and the closure of the South Tian Shan Ocean [START_REF] Carroll | Late Paleozoic tectonic amalgamation of northwestern China: sedimentary record of the northern Tarim, northwestern Turpan, and southern Junggar basins[END_REF][START_REF] Chen | Closing history of the southern Tianshan oceanic basin, western China: an oblique collisional orogeny[END_REF][START_REF] Liu | Petrology and geochemistry of Early Permian volcanic rocks in South Tian Shan, NW China: implications for the tectonic evolution and Phanerozoic continental growth[END_REF][START_REF] Alexeiev | Tectono-stratigraphic framework and Palaeozoic evolution of the Chinese South Tianshan[END_REF]. During that period, the Tarim Basin evolved as a compressive basin with Upper Carboniferous to Lower Permian series consisting of marine limestones, volcanoclastics and continental conglomerates, sandstones and siltstones (Caroll et al., 1995;[START_REF] Lin | Distribution and erosion of the Paleozoic tectonic unconformities in the Tarim Basin, Northwest China: significance for the evolution of paleo-uplifts and tectonic geography during deformation[END_REF].

Subsequent Early Permian extension then occurred and was associated to the emplacement of a LIP province within the basin [START_REF] Carroll | Late Paleozoic tectonic amalgamation of northwestern China: sedimentary record of the northern Tarim, northwestern Turpan, and southern Junggar basins[END_REF][START_REF] Qin | SIMS zircon U-Pb geochronology and Sr-Nd isotopes of Ni-Cu-Bearing Mafic-Ultramafic Intrusions in Eastern Tianshan and Beishan in correlation with flood basalts in Tarim Basin (NW China): Constraints on a ca. 280 Ma mantle plume[END_REF][START_REF] Yu | Permian flood basalts from the Tarim Basin, Northwest China: SHRIMP zircon U-Pb dating and geochemical characteristics[END_REF].

A C C E P T E D M A N U S C R I P T

During the Mesozoic, the Tarim Basin finally seems to evolve again as a compressive basin in its northern and eastern parts [START_REF] Desheng | Hydrocarbon accumulations in the Tarim basin, China[END_REF], with Triassic, Jurassic and Early Cretaceous depositional systems consisting of alluvial plain to lacustrine environments [START_REF] Desheng | Hydrocarbon accumulations in the Tarim basin, China[END_REF][START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]. However, there are no Mesozoic deposits to the south-west of the basin, except along the Pamir-Western Kunlun Range, where Jurassic deposits are interpreted to have been deposited in pull-apart basins (Sobel et al., 1999).

4. The Fergana Basin

The Fergana Basin is an intracontinental basin situated to the west of the Kyrgyz Tian Shan. It is surrounded by the Chatkal and Kurama ranges to the north, the Fergana Range to the east and by the Alai Range to the south (Fig. 1). In its thickest part, it contains around 10 km of Permian to Quaternary sediments.

Following the late Paleozoic building of the ancestral Tian Shan, post-orogenic Upper

Permian to Lower Triassic alluvial to lacustrine sediments were deposited [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF]Moisan et al., 2011). The basin was then subsequently inverted leading to a Middle -Late

Triassic erosional event [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF][START_REF] Bande | Cenozoic palaeoenvironmental and tectonic controls on the evolution of the northern Fergana Basin[END_REF]. Renewed subsidence started from the Early Jurassic and led to the accumulation of alluvial to lacustrine deposits during the Jurassic and Early Cretaceous [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF]Jolivet et al., 2017a;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

5. The Yarkand -Fergana Basin

The Yarkand -Fergana Basin is described as a transtensional pull-apart basin located along the south-western termination of the Talas Fergana/Karatau fault (Fig. 1) (Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Alexeiev et al., 2017;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. The sedimentary

A C C E P T E D M A N U S C R I P T

thickness progressively decreases away from the fault where up to 5 km of Jurassic sediments were deposited (Sobel et al., 1999;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Lower to Middle Jurassic sediments consist mainly of alluvial, fan delta and deep lake deposits containing coal beds and plant fragments indicating humid conditions (Sobel et al., 1999;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

To the south of the basin, in the north-western Tarim region, the Upper Jurassic -Lower

Cretaceous transition consists in up to 400 m-thick conglomeratic fluvial channel systems subsequently followed by Lower Cretaceous deposits characterized by fluvial red beds (Sobel et al., 1999).

SEDIMENTOLOGICAL ANALYSES

1. METHODS AND AGE CONSTRAINTS

In this study we present new sedimentological data from Upper Triassic to Lower Cretaceous sedimentary units from the south Junggar, north Tarim, Yili and Bayanbulak basins (Fig. 1; see Appendix A for GPS coordinates of analyzed sections). Detailed analyses of field logs (1/1000 scale), sedimentary facies, trace fossils and paleosols were performed on each of the seven sections presented below with the objective of reconstructing the depositional environment evolution through time.

To establish the first order age intervals in the sediment sequences and assess the corresponding formation names (Fig. 2; lithostratigraphy from [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF],we relied on geological maps (XBGMR, 1969(XBGMR, , 1970(XBGMR, , 1973(XBGMR, a, b, 1978 a, b) a, b), published ages derived from biostratigraphical analyses and sporopollen assemblages (for more references see [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF] and published lithological descriptions [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF].

A C C E P T E D M A N U S C R I P T 13

2. FACIES MODEL AND DEPOSITIONAL ENVIRONMENTS

In the seven sections described below, twelve facies assemblages were defined based on lithology and sedimentary structures before being interpreted in terms of depositional processes (Table . 1). Together with those facies, five different pedogenic and alteration features were also identified (Table . 2). All these facies, pedogenic and alteration features were subsequently associated and interpreted in terms of depositional environments (Table .     3). Climatic conditions were inferred from these sedimentological analyses. In total, 10 environments ranging from alluvial fan to lake, evolving in both humid and semi-arid/arid conditions have been defined. 3D diagrams have been constructed to illustrate the general organization of each proposed depositional environment (Table . 3).

However, some morphological variability exists within those environments, especially for the lacustrine delta systems. Indeed, lithologies and sedimentary structures vary depending on the sections and are, for example, characteristic of different flow regimes. For the purpose of this paper we decided to group these more specific morphologies within one general environment associated with a global architecture (i. e. lacustrine delta (LD), Table . 3). Sediment-charged flash floods due to either seasonal or irregular rainfalls (e.g., [START_REF] Blair | Alluvial fans and their natural distinction from rivers based on morphology, hydraulic processes, sedimentary processes and facies assemblages[END_REF].

Occasional sheet flow and stream flow deposits [START_REF] Miall | Lithofacies types and vertical profile models in braided river deposits: a summary[END_REF])

F13

a m-to pluri m-thick conglomerates with subangular to subrounded pebbles to boulders, poorlysorted, matrix-supported (sand-rich)

Massive, sometimes with faint horizontal laminations. Erosive or sharp basal boundaries Gravity flow processes, Debris flows [START_REF] Postma | Depositional architecture and facies of river and fan deltas: a synthesis[END_REF][START_REF] Miall | The Geology of Fluvial Deposits[END_REF]

Table. 2: Description and interpretation of pedogenic and alteration features

336

Facies code

Lithology Interpretations

P1

Closely spaced, disconnected thin vertical root traces, mm in thickness and a few cm-long within siltstones to fine grained sandstones Paleosols [START_REF] Retallack | Field recognition of palaeosols[END_REF])

P2

Sparse vertical roots, mm wide, a few cm to dmlong within sandstones Patchy and discontinuous vegetation typical of dry climate conditions (e.g., [START_REF] Hasiotis | Climatic controls on continental track fossils[END_REF]

P3

Siltstone and sandstone facies modified by marmorisation processes Pseudo-hydromorphic palaeovertisoils, wet-dry climate [START_REF] Kraus | Paleosols in clastic sedimentary rocks: their geologic applications[END_REF][START_REF] Klappa | Rhizolites in terrestrial carbonates: classification, recognition, genesis and significance[END_REF][START_REF] Hasiotis | Climatic controls on continental track fossils[END_REF])

P4

Dispersed to coalescent calcareous nodules, a cmto several cm in diameter within siltstones to fine grained sandstones

Semi-arid pedogenic processes indicative of seasonality (wetdry conditions; e.g., [START_REF] Retallack | Field recognition of palaeosols[END_REF][START_REF] Hasiotis | Climatic controls on continental track fossils[END_REF] P5 m-to several m-thick calcareous impregnation/cementation within conglomerates

Long-lasting wet/dry pedogenic processes within semi-arid environment (e.g., [START_REF] Retallack | Field recognition of palaeosols[END_REF]2008) Table . 3: Summary of the characteristics of the associated facies and their interpretations in

1. 1. South Toutunhe section

The South Toutunhe section (Fig. 6) is located in the south Junggar Basin, along the Toutun River on the northern flank of the Tian Shan Range and more precisely to the south of the Toutun dam (Fig. 1; Appendix B for a general overview of the section). The studied ~2000 m-thick section covers Middle Jurassic (Toutunhe Fm), Upper Jurassic (Qigu and Kalaza fms), and Lower Cretaceous (Qingshuihe Fm) deposits (XBGMR, 1978b).

A C C E P T E D M A N U S C R I P T 20

The basal part of the logged Toutunhe Fm consists of distal alluvial plain deposits associated to coal beds indicative of rather humid conditions (AP2) (Table . 3), which pass upward, in the last 230 m of the formation to lacustrine delta deposits (LD) (Fig. 6

1. 2. North Toutunhe section

The North Toutunhe section (Fig. 7) is also located along the Toutun River, to the north of the Toutun dam (Fig. 1; Appendix C for a general overview of the section) and presents ~1650 m of deposits ranging from Late Jurassic (Qigu and Kalaza fms) to Early Cretaceous (Qingshuihe Fm) in age (XBGMR, 1978b). Indeed the Kalaza Fm (~740 m thick) consists of large aeolian dunes (preserved dune sets are up to 50 m in thickness) and interdune deposits characteristic of erg systems (EG) (Fig. 7).

The basal part of the Lower Cretaceous Qingshuihe Fm shows a drastic change in environments with the emplacement of sediments indicative of lacustrine delta (LD) followed by lacustrine deposits (LE1) dominated by fine -grained facies.

1. The Manas section

The ~5510 m-thick Manas section (Fig. 8), located in the south Junggar Basin, along the Manas River on the northern flank of the Tian Shan Range (Fig. 1; Appendix D for general pictures of the section) encompasses Upper Triassic, Lower Jurassic (Badaowan and Sangonghe fms), Middle Jurassic (Xishanyao and Toutunhe fms), Upper Jurassic (Qigu and Kalaza fms) and Lower Cretaceous (Qingshuihe Fm) deposits (XBGMR, 1978a;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF].

The upper part of the Triassic succession (only the topmost ~200 m were logged in this work) displays distal alluvial plain (AP2) and lacustrine delta environments (LD) evolving towards alluvial fan systems (AF) (Fig. 8). The first 780 m of the Lower Jurassic series (Badaowan Fm) consists of an alternation of distal alluvial plain (AP2) and alluvial fan (AF) deposits. The latter are dominated by clast-supported conglomerates with sub-rounded pebbles, occasionally associated with coal beds, which suggest rather humid conditions (AF) (Fig. 8; Appendix D. 1). These deposits pass upwards in a retrogradational trend into sediments indicative of a lacustrine delta environment (LD). Above, the top 400 m of the Lower Jurassic series correspond to the Sangonghe Fm, which is characterized by a progradational trend towards a proximal alluvial plain system (AP1) followed by a Fm is sharp with environments retrograding sharply toward a lacustrine system (LE1).

A C C E P T E D M A N U S C R I P T

1. 4. The Wusu section

The Wusu section (Fig. 9) is also located on the southern Junggar Basin, to the south of the Wusu City on the northern flank of the Tian Shan Range (Fig. 1; Appendix E for a general overview of the section). Based on the geological map (XBGMR, 1978a), this ~1650 m-thick section encompasses Middle (Xishanyao and Toutunhe fms) to Upper Jurassic (Qigu and Kalaza fms) deposits. The lower and upper parts of this sedimentary section (up to the Qigu Fm) have been respectively logged in the west and east of Saili Keti village (Appendix A for GPS coordinates), with a few meters of overlap expected between them.

The first 190 m of the Xishanyao Fm correspond to alluvial fan deposits (AF)

retrograding sharply towards a ~85 m-thick unit of lacustrine sediments (LE1) (Appendix E.

1, 2). This unit marks the onset of a 200 m-thick progradational trend with depositional environments evolving from a lacustrine delta (LD) to more and more proximal alluvial plains (AP2, AP1), followed by an alluvial fan system (AF) (Fig. 9; Appendix E. 3). The upper part of the Xishanyao Fm then consists of alluvial fan (AF) and proximal alluvial plain (AP1) deposits. These proximal alluvial deposits are still present in the lower part of the Toutunhe Fm and pass upward into sediments deposited in a more distal alluvial plain environment (AP2) in a retrogradational trend (Fig. 9; Appendix E. 4, 5). Both the Middle Jurassic Xishanyao and the Toutunhe fms contain several tuffaceous beds (cm to dm thick) indicating volcanic activity as well as numerous coal beds associated with alluvial plain deposits indicating rather humid climate conditions. Above, the lower part of the Upper Jurassic Qigu Fm consists of red siltstones and sandstones displaying root traces and interpreted as proximal alluvial plain (AP1) deposits (Appendix E. 6). The upper Qigu Fm displays alluvial fan deposits (AF) retrograding towards proximal alluvial plain (AP1) to distal alluvial plain (AP2a) deposits containing carbonate nodules indicating semi-arid climatic conditions (Fig. 9). The Qigu Fm ends with a sharp boundary marking the transition between the deposits of a

A C C E P T E D M A N U S C R I P T

proximal alluvial plain environment (AP1) and the 150 m-thick Kalaza Fm (Fig. 9). The latter is dominated by planar to sub-planar laminated conglomerates (Appendix E. 7) interpreted as an alluvial fan sediments deposited in semi-arid conditions (AFa). Finally, the transition between the Kalaza Fm and the basal part of the Qingshuihe Fm is marked by a rapid retrogradation towards a distal alluvial plain environment (AP2).

2. Intra-mountain basins

2. 1. The Nieleke section

The Nieleke section (Fig. 10) is situated in the Tian Shan Range within the Hexilagen Basin (Fig. 1; Appendix F for a general overview of the section) and covers ~925 m of Middle Jurassic (Toutunhe Fm) deposits (XBGMR, 1978b).

The first 310 m of the section consist mostly of interbedded siltstones and sandstones associated with coal deposits and interpreted to be deposited in a lacustrine delta (LD).

Several oxidized paleosols are also visible in the bottom part of this unit (Fig. 10; Appendix F. 1) suggesting warm and humid climatic conditions. The next 410 m show successive retrogradational and progradational trends with depositional environments evolving from a distal alluvial plain (AP2) to a lacustrine delta (LD) and back to a distal alluvial plain (AP2) deposits (Fig. 10; Appendix F. 2). The upper part of the section is characterized by a 50 mthick unit of stacked, coarse-grained to gravelly sandstone beds interpreted to be lacustrine delta deposits (LD) (Fig. 10). This marks the onset of a progradational trend from a lacustrine delta (LD) to more and more proximal alluvial plain environments (AP2, AP1) (Appendix F.

3).

A C C E P T E D

M A N U S C R I P T 25

2. 2. The Bayanbulak section

The Bayanbulak section (Fig. 11) is situated in the Tian Shan Range, in the northern part of the Bayanbulak Basin (Fig. 1; Appendix G for a general overview of the section). It presents ~420 m of Middle Jurassic deposits (XBGMR, 1969), which we attribute to the Toutunhe Fm based on their lithology.

The lowest ~70 m of sediments of this section indicate a proximal alluvial plain environment (AP1) with several coal deposits. They pass upward into alluvial fan deposits (AF) (Appendix G. 1). The rest of the succession is characterized by an alternation between proximal alluvial plain (AP1) and alluvial fan (AF) deposits (Fig. 11). The last ~20 m of the section are attributed to the Paleogene (XBGMR, 1969;[START_REF] Heilbronn | Stable isotope characterization of pedogenic and lacustrine carbonates from the Chinese Tian Shan: constraints on the Mesozoic-Lower Cenozoic palaeoenvironmental evolution[END_REF] and comprise red conglomerates impregnated/cemented by limestone (Appendix G. 2, 3) interpreted to be calcrete formed by long-lasting pedogenic processes within semi-arid, seasonal climates (see table 2).

The north Tarim Basin

1. The Yaha section

The Yaha section (Fig. 12) is located in the Kuqa depression, of the north Tarim Basin along the Yaha River on the southern flank of the Tian Shan Range (Fig. 1; Appendix H for a general overview of the section). This ~1525 m-thick section encompasses Lower Jurassic (Yengisar Fm), Middle Jurassic (Kezilenuer and Kalemake fms), Upper Jurassic (Qigu and Kalaza fms), and Lower Cretaceous (Yageliemu Fm) deposits (XBGMR, 1970;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF].

A C C E P T E D M A N U S C R I P T

The Yengisar Fm (~100 m-thick) consists of stacked, thick bedded gravelly sandstones interpreted as lacustrine delta deposits (LD) (Appendix H. 1, 2). They evolve, at the base of the Kezilenuer Fm, towards distal alluvial plain deposits (AP2) and finally back to lacustrine delta sediments (LD) in the upper part of this formation (the last 325 m) (Fig. 12; Appendix H. 3, 4). The base of the Kalemake Fm (~230 m) still consist of lacustrine delta deposits (LD)

retrograding toward lacustrine environments characterized by the presence of calcareous beds with some turbiditic events in the top ~200 m of the formation (Appendix H. 5). Their oxygen and carbon isotope compositions are typical of lacustrine carbonates [START_REF] Heilbronn | Stable isotope characterization of pedogenic and lacustrine carbonates from the Chinese Tian Shan: constraints on the Mesozoic-Lower Cenozoic palaeoenvironmental evolution[END_REF].

These observations seem to indicate a rather deep lacustrine environment (LE1) in comparison to lake environments encountered in the previous sections. Middle Jurassic units are also associated to numerous coal beds indicating humid climate conditions. The Qigu Fm (~200 m in thickness) is characterized by a thick red-bed series (Appendix H. 6) interpreted as playa lake deposits (LE1a) prograding towards more and more proximal alluvial plain deposits associated to carbonate nodules that indicate semi-arid climate conditions (AP2a, AP1a). Above, the Kalaza Fm is particularly thin (~35 m) in comparison to other sections and consists of alluvial fan deposits (AFa) (Fig. 12; Appendix H. 7). Finally, the lower part of the Lower Cretaceous Yageliemu Fm is characterized by proximal to distal alluvial plain sediments deposited under semi-arid conditions (AP2a, AP1a) (Appendix H. 8). Within the upper part of the section, the sediments evolve towards deposits associated to a more distal lacustrine delta environment (LD).

JURASSIC PALEOGEOGRAPHICAL EVOLUTION OF THE TIAN SHAN

As mentioned above, the present-day geometry of the range results from a series of Meso-Cenozoic reactivations of late Paleozoic tectonic structures (e.g., Molnar and Taponnier, 1975;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Sobel et al., 1999;[START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF]; [START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]. However, the exact pattern of Cenozoic deformation in the Tian Shan Range is still poorly understood. The total Cenozoic shortening is estimated to be 124 ± 30 km at the longitude of Manas (ca. 85,5° E; Chinese Tian Shan) and 203 ± 50 km at the longitude of Kashgar (ca. 76° E; Kyrgyz Tian Shan) [START_REF] A C C E P T E D M A N U S C R I P T 52 Avouac | Active Thrusting and Folding Along the Northern Tien Shan and Late Cenozoic Rotation of the Tarim Relative to Dzungaria and Kazakhstan[END_REF]. Though, this deformation is distributed on a number of faults, the exact kinematics of which being poorly constrained with likely significant strike-slip displacements. In addition, no Mesozoic deformation estimates are available. Due to this lack of kinematic constraints, we decided not to attempt to palinspastically restore the proposed paleogeographic maps.

A C C E P T E D M A N U S C R I P T

1. EARLY -EARLY MIDDLE JURASSIC

The Early to early Middle Jurassic paleogeography of the Tian Shan region was characterized by the presence of several sedimentary basins separated by significant reliefs (Fig. 13).

In the northeastern Junggar Basin (Kelameili region), the sedimentation was dominated by alluvial fan and alluvial plain deposits [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF], indicating the existence of an eroding relief to the east within the vicinity of the present-day Altai Range. Indeed, Upper Triassic and Lower Jurassic angular unconformities were associated with coarse-grained pulses in the sedimentation suggesting that episodes of deformation and erosion took place in this area [START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. This is in agreement with seismic data showing that this region underwent transpressional deformation during Early Jurassic times [START_REF] Zhao | Intracontinental orogenic transition: Insights from structures of the eastern Junggar Basin between the Altay and Tianshan orogens[END_REF]. To the south-east, sedimentation in the Junggar and Turfan basins consisted mainly of alluvial to lacustrine deposits.

Widespread perennial lakes and associated lacustrine deltas developed within the central part of both basins while alluvial environments dominated in the areas nearby the reliefs (this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Shao et al., 2003;[START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Feng | Sequence stratigraphy, sedimentary systems and petroleum plays in a low-accommodation basin: Middle to upper members of the Lower Jurassic Sangonghe Formation, Central Junggar Basin, Northwestern China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. Paleocurrent measurements together with sedimentological and provenance analyses seem to indicate the presence of a low relief between the Junggar and Turfan basins (the present day Bogda Shan area) [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Greene | Sedimentary record of Mesozoic deformation and inception of the Turpan-Hami basin, northwest China[END_REF]Shao et al., 2003;[START_REF] Roger | Late Paleozoic to Jurassic tectonic evolution of the Bogda area (northwest China): Evidence from detrital zircon U-Pb geochronology[END_REF]. However, the lack of Early Jurassic ages in the low-temperature thermochronology data of the Bogda Shan area indicates the absence of significant tectonic exhumation [START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF]. This suggests that the relief was not derived from an Early Jurassic uplift and deformation event, but was probably inherited from the Permian to Triassic topography.

In the western Junggar Basin (Karamay region), several unconformities within the Lower Jurassic series are directly followed by conglomerate deposits (Eberth et al., 2010;[START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF]Ma et al., 2014) and indicate that several deformation events also occurred in this area. The presence of alluvial fan and alluvial plain environments [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF] together with braided delta prograding eastward into a lake [START_REF] Feng | Sequence stratigraphy, sedimentary systems and petroleum plays in a low-accommodation basin: Middle to upper members of the Lower Jurassic Sangonghe Formation, Central Junggar Basin, Northwestern China[END_REF], point again to the existence of an eroding relief in place of the present day Halaalate mountains which provided sediments to the Junggar Basin.

Along the southern margin of the Junggar Basin, depositional environments consisted of alluvial fans to alluvial plains. The occurrence of numerous coal beds together with plant remnants in the associated series suggests rather humid conditions (this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF].

W hus p opos h h "Waagenoperna" d sc ib d in h Jun

Basin is most likely a misidentified freshwater bivalve of unknown affinities and that no marine incursion occurred in the southern area of the Junggar Basin during the Early Jurassic epoch.

Along the Manas section (Fig. 1 for location; Fig. 8), the unconformity between the Upper Triassic and Lower Jurassic sediments suggests that deformation and erosion events took place at the southern margin of the Junggar Basin during this period [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. North directed paleocurrent measurements together with provenance data indicate that these sediments were derived from the south, locating a relief in the place of the present day Tian Shan Range [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF]. These observations are in agreement with low-temperature thermochronology data which highlight a Late Triassic -Early Jurassic cooling phase associated with the reactivation of the main Paleozoic structures of the North Tian Shan region [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF].

Several intra-mountain basins were also active within the Tian Shan Range during the Early to early Middle Jurassic. The Yili Basin was principally occupied by alluvial plain, lacustrine delta and lacustrine environments with coal deposits suggesting humid conditions.

The main depocenter was located in the northern part of the basin [START_REF] Li | Geological controls on coal quality of the Yili Basin, Xinjiang Northwest China[END_REF]. To the south, the Zahosu depression was also active [START_REF] Li | Dynamic processes from plate subduction to intracontinental deformation: Insights from the tectono-sedimentary evolution of the Zhaosu-Tekesi Depression in the southwestern Chinese Tianshan[END_REF]. Coarse grained fan delta deposits prograding towards the north in the Yili Basin [START_REF] Li | Geological controls on coal quality of the Yili Basin, Xinjiang Northwest China[END_REF] and the sediment grain-size evolving southward from conglomerates to sandstones and siltstones in the Zahosu depression [START_REF] Li | Dynamic processes from plate subduction to intracontinental deformation: Insights from the tectono-sedimentary evolution of the Zhaosu-Tekesi Depression in the southwestern Chinese Tianshan[END_REF] imply that a physiographic separation existed between the two basins at that time. To the south-east, preserved Lower Jurassic sediments along the northern edge of the Bayanbulak Basin (XBGMR, 1969) suggest that this depression was also active during this period. Finally a Late Triassic -Early Jurassic cooling phase was identified in the low-temperature thermochronology data along the Narat Range between the Bayanbulak and

A C C E P T E D M A N U S C R I P T 30

Yili basins. This suggests the presence of an eroding relief separating these basins [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF].

To the south-east of the Tian Shan, the Yanqi Basin presents deposits associated to environments evolving from alluvial fan to lacustrine systems (Al-Qaraafi and Guangqing, 2013). Sedimentological analyses within both the Turfan and Yanqi basins suggest that they were separated from each other by an eroding relief (Shao et al., 2003;Al-Qaraafi and Guangqing, 2013). However, whether the Yanqi and Tarim basins were connected or separated by a relief during the Early to early Middle Jurassic is unclear due to the lack of data in that region.

During this period, the north Tarim Basin was characterized by alluvial fan systems evolving southward to alluvial plain, lacustrine delta and lacustrine environments (Fig. 12).

Provenance analyses together with south directed paleocurrents indicate the existence of an eroding relief to the north forming the main source area for the detrital material deposited in this part of the basin [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Li | Detrital zircon geochronology and its provenance implications: responses to Jurassic through Neogene basin-range interactions along northern margin of the Tarim Basin, Northwest China[END_REF][START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF][START_REF] Wang | Continuous denudation and pediplanation of the Chinese Western Tianshan orogen during Triassic to Middle Jurassic: Integrated evidence from detrital zircon age and heavy mineral chemical data[END_REF]. The very monogenic (quartz) and well-sorted grain size of the lacustrine delta sediments encountered in the Yaha section (Yengisar Fm; Fig. 12) could indicate that these deposits were possibly reworked from an old weathering profile. This statement is in agreement with the provenance data [START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF] which indicate that topography of the source area could have already been partially flattened at that time.

To the west of the Tian Shan, in the Fergana Basin, renewed subsidence occurred during the Early Jurassic following the erosion event that characterized the Triassic period in that region [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF]. This led to the accumulation of 90-400 m-thick deposits in alluvial, lacustrine fan delta to shallow lacustrine environments, which unconformably overlay the Paleozoic basement [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Numerous coal beds and plant remnants were described in these deposits indicating abundant vegetation and humid climate conditions. At the same time, to the east of the Fergana Basin, ~4000 m of

A C C E P T E D M A N U S C R I P T

31 sediments were deposited within the Yarkand-Fergana Basin (Sobel et al., 1999). This strong sediment accommodation is thought to be induced by strike-slip motion on the Talas Fergana/Karatau fault leading to the formation of an Early -Middle Jurassic pull-apart basin (Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Alexeiev et al., 2017) 1992) located within the northern part of the present day Kyrgyz Tian Shan (Fig. 1 for location). Generally, the stratigraphic ages of these sediments reported on the geological maps are Lower Jurassic (e.g., [START_REF] Lasovskiy | collisional s ik -s ip d fo m ions in Ti nsh n nd y E s n Xinji n[END_REF], however, no biostratigraphic data are available for these series. Sedimentation mainly consisted of alluvial plain, fan delta and shallow lacustrine deposits. These deposits are often associated with coal-rich layers and plant fragments indicating humid climate conditions although some caliche-type paleosols more typical of semi-arid conditions were also identified in the south Issyk-Kul Basin [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF][START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]. Low-temperature thermochronology data support a Middle Triassic -Early Jurassic cooling phase within the basement separating all these basins (e.g., De Grave et al., 2011;[START_REF] Glorie | Tectonic history of the Kyrgyz Sou h Ti n Sh n ( b shi-Iny ch k) su u zon : Th o of inh i d s uc u s du in d fo m ion-p op ion T c onics[END_REF] indicating the presence of eroding reliefs between these intra-mountain basins.

To the north of the Kyrgyz Tian Shan, no Lower Jurassic sediments have been described within the south Chu-Sarysu and Yili-Balkhash basins (VNIGNI and Beicip

A C C E P T E D M A N U S C R I P T 32

Franlab , 1992;AGMCA, 2008). We propose that these domains were dominated by sediment by-pass (i. e. lowland areas dominated by soil alteration, low erosion and/or low sedimentary export or by a poor preservation of thin sediment deposits) during the Earlyearly Middle Jurassic. Similarly, no Jurassic sediments have been deposited in the western part of the Tarim Basin, except for Jurassic series exposed more to the south, along the West Kunlun -Pamir Range (Lee 1985a, b;Sobel et al., 1999;[START_REF] Yang | Middle-Late Jurassic tectonostratigraphic evolution of Central Asia, implications for the collision of the Karakoram-Lhasa Block with Asia[END_REF]. We thus propose that this domain was also dominated by sediment by-pass during the Earlyearly Middle Jurassic.

Nevertheless, some restricted piedmonts deposits could have existed that were not preserved within the stratigraphic record.

2. LATE MIDDLE -EARLY LATE JURASSIC

The late Middle to early Late Jurassic paleogeography of the Tian Shan region was mostly characterized by sedimentary basins surrounded by relatively low-relief basement areas (Fig. 14).

In the northeastern Junggar Basin (Kelameili region), the late Middleearly Late Jurassic strata consist mainly of alluvial plain to shallow lacustrine deposits [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. These environments are more distal compared to the Early Jurassic ones and potentially indicate a lowering or a retreat further to the east of the Early Jurassic relief. However, some local Middle Jurassic unconformities have been identified in this area which suggests recurrent periods of localized deformation and erosion [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. To the north-east, in the Junggar and Turfan basins, late Middleearly Late Jurassic deposits reflect alluvial to lacustrine depositional environments (this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Shao et al., 2003;[START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. The paleocurrent measurements, sedimentological analyses and provenance studies indicate the presence of an existing relief between the two basins persisting from the Early Jurassic [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Shao et al., 1999Shao et al., , 2003;;[START_REF] Roger | Late Paleozoic to Jurassic tectonic evolution of the Bogda area (northwest China): Evidence from detrital zircon U-Pb geochronology[END_REF][START_REF] Ji | Early to Middle Jurassic tectonic evolution of the Bogda Mountains, Northwest China: Evidence from sedimentology and detrital zircon geochronology[END_REF]. Based on provenance studies, some authors proposed that this area also underwent several uplift episodes during the Middle Jurassic [START_REF] Roger | Late Paleozoic to Jurassic tectonic evolution of the Bogda area (northwest China): Evidence from detrital zircon U-Pb geochronology[END_REF][START_REF] Ji | Early to Middle Jurassic tectonic evolution of the Bogda Mountains, Northwest China: Evidence from sedimentology and detrital zircon geochronology[END_REF]. However, the lack of contemporaneous exhumation ages and the occurrence of fine grained sediments in both the Junggar and Turfan basins rather suggest the absence of strong exhumation events in this region (Shao et al., 2003;[START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF].

To the west of the Junggar Basin (Karamay region), the sedimentation was dominated by alluvial fan to alluvial plain deposits [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF]. The presence of a Middle Jurassic unconformity sealed by conglomerates again indicates that deformation persisted in that area during this period [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF].

Along the southern margin of the Junggar Basin, the strata exposed in the Wusu section consist mainly of alluvial fan to alluvial plain deposits (Fig. 9). Further east, along the Manas and Toutunhe sections, the sediments are characteristic of more distal environments such as alluvial plain to lacustrine delta (Figs. 6, 7, 8) (this study;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF]. North-oriented paleocurrents attest of the presence of an eroding relief to the south [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]. The more distal depositional environments in the Manas region potentially indicate that this relief was lower or located further south than during the Early Jurassic. This trend is in agreement with the low-temperature thermochronology data which associate the Middle Jurassic to a period of low basement cooling rates and thus to a period of flattening of the relief in the North Tian Shan region [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]. In the southern margin of the Junggar Basin, the late Middle Jurassic deposits contain numerous coal beds (Figs. 6, 7, 8) (this study;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF]. The occurrence of these coal beds indicates that rather humid conditions persisted during that period. This coal disappears in the early Late Jurassic deposits, while extensive calcareous paleosols indicative of semi-arid conditions developed (This study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Deng | The Jurassic System of Northern Xinjiang, China[END_REF]Jolivet et al., 2017a). Several volcanic tuff layers and syn-sedimentary volcanic zircons have also been described in the Middle Jurassic series along the southern margin of the Junggar Basin (Wusu and Manas sections, Bogda Shan) indicating a volcanic activity within the north Tian Shan region during that period (Fig. 9; [START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF]Simonov et al., 2015;[START_REF] Ji | Early to Middle Jurassic tectonic evolution of the Bogda Mountains, Northwest China: Evidence from sedimentology and detrital zircon geochronology[END_REF]. However, the eruption center has not yet been located.

The Middle Jurassic sediment in the Yili Basin consists of alluvial to lacustrine deposits (Fig. 10; [START_REF] Li | Geological controls on coal quality of the Yili Basin, Xinjiang Northwest China[END_REF]. Due to the absence of coarse grained sediments and to the presence of extensive coal beds in the southern part of the basin as well as in the Zahosu depression immediately to the south [START_REF] Li | Geological controls on coal quality of the Yili Basin, Xinjiang Northwest China[END_REF][START_REF] Li | Dynamic processes from plate subduction to intracontinental deformation: Insights from the tectono-sedimentary evolution of the Zhaosu-Tekesi Depression in the southwestern Chinese Tianshan[END_REF], we suggest that no erosive domain separated these two basins during that period. However, the occurrence of alluvial fan to proximal alluvial plain deposits in the northern part of the Bayanbulak Basin (Fig. 11)

implies the existence of a nearby eroding relief. Moreover, low-temperature thermochronology data indicate a Middle Jurassic period of slow cooling in the Narat region interpreted as a period of slow erosion [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]. We thus propose that the relief established along the Narat fault during the Late Paleozoic -Early Jurassic was not entirely flattened by Middle Jurassic and therefore, that it still constituted a physiographic separation between the Bayanbulak and Yili basins.

To the south-east of the Tian Shan, no data are available for the Middle -Late Jurassic strata of the Yanqi Basin. However, sedimentological analyses within the Turfan Basin indicate the presence of an eroding relief separating the Turfan Basin from the Tarim Basin (Shao et al., 2003).

Along the Yaha section in the north Tarim Basin, the Middle Jurassic strata were deposited in alluvial plain to lacustrine environments (Fig. 12). South-directed paleocurrents and provenance analyses also indicate the presence of an eroding relief to the north [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Li | Detrital zircon geochronology and its provenance implications: responses to Jurassic through Neogene basin-range interactions along northern margin of the Tarim Basin, Northwest China[END_REF][START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF][START_REF] Wang | Continuous denudation and pediplanation of the Chinese Western Tianshan orogen during Triassic to Middle Jurassic: Integrated evidence from detrital zircon age and heavy mineral chemical data[END_REF]. However, the more distal depositional environments compared to the Early Jurassic ones suggest a lowering or a

A C C E P T E D M A N U S C R I P T

35 northward retreat of the relief with a widening of the basin. This is also supported by detrital zircon U-Pb data showing a widening of the sediment source area during the Middle Jurassic [START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF].

To the west of the Tian Shan, the Middle Jurassic series in the Fergana Basin consist of 100-300 m-thick alluvial to lacustrine deposits [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

Coal beds and plant fragments are abundant within these sediments and indicate humid conditions [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. To the east of the Fergana Basin, the Yarkand-Fergana Basin was still subsiding due to strike-slip motion along the Talas Fergana/Karatau fault and it accommodated ~600-1550 m of Middle Jurassic sediments (Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Alexeiev et al., 2017). The facies of the latter indicate the occurrence of alluvial plain, lacustrine delta and lacustrine depositional environments (Sobel et al., 1999;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Like in the Chinese Tian Shan, low-temperature thermochronology data indicate low cooling rates during the Middle Jurassic within the Kyrgyz Tian Shan. This was interpreted as a period of slow erosion leading to progressive planation of the basement areas [START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2013;[START_REF] Macaulay | Cenozoic deformation and exhumation history of the Central Kyrgyz Tien Shan[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF].

Meanwhile, in the Ming-Kush, south Issyk-Kul, Naryn and Aksai basins, a Middle Jurassic to Eocene hiatus in sedimentation has been identified [START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF][START_REF] Burbank | Partitioning of intermontane basins by thrust-related folding, Tien Shan, Kyrgyzstan[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

Further north, no Middle -Late Jurassic sediments were described within the south Chu-Sarysu and Yili-Balkhash basins [START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]AGMCA, 2008).

We propose that these domains were still dominated by sediment by-pass during this period.

Similarly to the Early Jurassic period, the western Tarim Basin seems also dominated by sediment by-pass during the Middle -Late Jurassic (Lee 1985a, b). Nevertheless, some restricted piedmonts deposits could again have existed that were not preserved within the stratigraphic record.

3. LATE JURASSIC -EARLY CRETACEOUS TRANSITION

In the Tian Shan region, the Late Jurassic -Early Cretaceous transition corresponds to a drastic paleogeographic change in comparison to the Early and Middle Jurassic periods (Fig. 15). In the Junggar and Turfan basins, the sedimentation was dominated by alluvial fan to alluvial plain deposits [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Shao et al., 1999;[START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF]Jolivet et al., 2017a). Low-temperature thermochronology data indicate a Jurassic -Early Cretaceous fast cooling event in the present day Bogda Shan area implying that this region underwent deformation and uplift during this period [START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF].

To the north-east and north-west of the Junggar Basin, in the Kelameili and Karamay regions (Fig. 15), the Upper Jurassic -Lower Cretaceous deposits are associated with alluvial fans and alluvial plain environments [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Jolivet et al., 2017a). Angular unconformities at the base of the alluvial fans sediments (corresponding to the Kalaza Fm) have been identified in both regions and are, in the Kelameili area, associated with incised paleo-valleys [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF]. They imply uplift and relief building in these areas, in agreement with the seismic data indicating that transpressive deformation occurred within the eastern and western part of the Junggar Basin during the Jurassic [START_REF] Zhao | Intracontinental orogenic transition: Insights from structures of the eastern Junggar Basin between the Altay and Tianshan orogens[END_REF][START_REF] Yu | Mesozoic reactivated transpressional structures and multi-stage tectonic deformation along the Hong-Che fault zone in the northwestern Junggar Basin, NW China[END_REF]. Such a tectonic setting could have led to widespread deformation leading to the generation of a relief within the Junggar Basin.

Indeed, a NE-SW-orientated erosional area, the Chemo uplift, started to develop within the central part of the Junggar Basin during the Middle Jurassic and reached its peak stage during the Late Jurassic -Early Cretaceous [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF][START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF]. Erosion of this topographic high provided terrigenous material that was shed into the adjacent, still subsiding areas [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF][START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF].

Based on seismic data, [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF] estimated that the amplitude of this paleorelief could have reached 740 m during its peak development stage.

Along the southern margin of the Junggar Basin, the sedimentation consisted mainly of several meters to hundred meters-thick alluvial fan deposits typical of semi-arid to arid climate conditions (Figs. 6,8,9) (this study; Jolivet et al., 2017a). Indeed, aeolian deposits are present in the Kelameili and Toutunhe regions (Fig. 1 for location). Along the south Toutunhe section, they are interbedded with ephemeral alluvial fan deposits (Fig. 6) and evolved northward to erg deposits with large dunes and interdunes (Fig. 7). The occurrence of these thick aeolian deposits indicate that this region was under semi-arid to arid climate conditions during the Late Jurassic -Early Cretaceous (this study; [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Jolivet et al., 2017a).

As in the north of the Junggar Basin, angular unconformities have been identified at the base or within the Kalaza Fm (Hutubi and North Toutunhe sections) (this study; Jolivet et al., 2017a). Moreover, provenance analyses demonstrate that recycling of Mesozoic sediments took place in this area. These observations imply that some tectonic movements and rock uplift also occurred during the Late Jurassic -Early Cretaceous within the North Tian Shan foothills [START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF]. However, low-temperature thermochronology data on basement rocks from the central Tian Shan do not identify any evidence of tectonic movements during this period and show that exhumation was in fact controlled by slow erosion since the Middle Jurassic [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]. Accordingly, we propose that small amplitude tectonic movements occurred within the North Tian Shan Range and its piedmont, leading to limited relief building during the Late Jurassic -Early Cretaceous.

Within the Tian Shan Range, both Yili and Bayanbulak basins do not contain Upper Jurassic -Lower Cretaceous sediments (AGMCA, 2008). Following an Late Jurassic -Early Cretaceous unconformity, a ~40 m-thick weathered layer formed within the Yili Basin, overlain by Upper Cretaceous sediments and indicating rather stable conditions for a long

A C C E P T E D M A N U S C R I P T

period of time [START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]. Therefore, we propose that this domain was dominated by sediment by-pass during the Late Jurassic -Early Cretaceous. To the south, low-temperature thermochronology data indicate slow cooling, hence low erosion within the Narat Range. This suggests a continuous flattening of the topography during this period [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF]. In the Bayanbulak Basin, Eocene (?) strata rest unconformably on the Middle Jurassic series again implying that the basin was dominated by sediment by-pass and/or erosion during the Late Jurassic -Early Cretaceous.

To the south-east of the Tian Shan, the relation between the Yanqi and the Tarim basins is not clear. No Upper Jurassic -Lower Cretaceous sediments were described within the Yanqi Basin (AGMCA, 2008;[START_REF] Huang | Late Pleistocene shortening rate on the northern margin of the Yanqi Basin, southeastern Tian Shan, NW China[END_REF]. We therefore propose that this region was dominated by sediment by-pass during this period.

In the northern part of the Tarim Basin, the Late Jurassic -Early Cretaceous sedimentation was characterized by relatively thin alluvial fan deposits (in comparison to the Junggar Basin) evolving southward towards alluvial plain deposits (Fig. 15). Provenance and petrographic analyses point to a sediment source from the South Tian Shan Range, altogether with local recycling of Mesozoic sediments indicating a southward migration of the eroding topography [START_REF] Li | Mesozoic-Cenozoic tectonic relationships between the Kuqa subbasin and Tian Shan, northwest China: constraints from depositional records[END_REF][START_REF] Li | Detrital zircon geochronology and its provenance implications: responses to Jurassic through Neogene basin-range interactions along northern margin of the Tarim Basin, Northwest China[END_REF].

To the west, the Late Jurassic -Early Cretaceous sedimentation in the Fergana Basin consisted of alluvial fan and alluvial plain deposits (Fig. 15). In the northern part of the basin (Tash-Komyr section; Fig. 1), the transition between the Jurassic and the Cretaceous is marked by an erosional unconformity directly followed by > 110 m-thick alluvial fan deposits [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. This suggests that some tectonic movements occurred during that period. To the south (Jetim-Dobo section; Fig. 1) the sedimentation consists of alluvial plain deposits containing calcareous paleosols, and indicating semi-arid climate conditions [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

A C C E P T E D M A N U S C R I P T 39

Meanwhile to the east, alluvial fan and proximal alluvial plain systems developed in the western and southern parts of the Yarkand-Fergana Basin (Sobel et al., 1999;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Provenance studies on Late Jurassic -Early Cretaceous samples indicate potential recycling of older Jurassic sediments and smaller drainage area compared to the Early -Middle Jurassic paleogeography [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Together, these data imply a Late Jurassic -Early Cretaceous inversion of the Yarkand-Fergana Basin. This renewed tectonic activity is further supported by low-temperature thermochronology data which identify a Late Jurassic -Early Cretaceous cooling event in the Kyrgyz Tian Shan Range suggesting a localized relief building [START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2012, 2013;[START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

No Upper Jurassic -Lower Cretaceous sediments were described within the Chu-Sarysu, Yili-Balkash and west Tarim basins (Lee 1985a, b;[START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]AGMCA, 2008). We therefore propose that these domains were still dominated by sediment by pass during this period even though some restricted piedmont deposits could have existed and not subsequently preserved within the stratigraphic record.

DISCUSSION

1. TOPOGRAPHIC AND CLIMATIC EVOLUTION OF THE TIAN SHAN

The Jurassic topographic evolution of the Tian Shan was dominated by the progressive planation of a late Paleozoic to early Mesozoic relief, locally interrupted by discreet topographic rejuvenations (Fig. 16) (e.g., this study, [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF][START_REF] Li | Detrital zircon geochronology and its provenance implications: responses to Jurassic through Neogene basin-range interactions along northern margin of the Tarim Basin, Northwest China[END_REF][START_REF] Liu | Latest Paleozoic-Early Mesozoic basin-range interactions in South Tian Shan (northwest China) and their tectonic significance: Constraints from detrital zircon U-Pb ages[END_REF][START_REF] Macaulay | Cenozoic deformation and exhumation history of the Central Kyrgyz Tien Shan[END_REF]. In both the north and south Tian Shan foothills, a progressive transition can be observed from Early Jurassic coarse-grained sediments associated with proximal alluvial environments, to finer-grained deposits [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF]. This highlights the progressive decrease of the Tian Shan relief. During the Early to Middle Jurassic, the sedimentation, in the basins surrounding the range and in the intra-mountain depressions, was characterized by alluvial to lacustrine deposits containing numerous coal beds and plant fragments indicating humid climate conditions (Fig. 16; this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Sobel et al., 1999;[START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Finally, the Middle Jurassic period was also characterized by volcanic activity within the north Tian Shan region (this study; [START_REF] Yang | Source to sink relations between the Tian Shan and Junggar Basin (northwest China) from Late Palaeozoic to Quaternary: evidence from detrital U-Pb zircon geochronology[END_REF]Simonov et al., 2015;[START_REF] Ji | Early to Middle Jurassic tectonic evolution of the Bogda Mountains, Northwest China: Evidence from sedimentology and detrital zircon geochronology[END_REF]. During the early Late Jurassic, the Tian Shan relief was still decreasing, with contemporaneous fine-grained sediments deposited in distal alluvial to lacustrine environments. However, this period was marked by a change in climate conditions, recorded all over the Tian Shan area by the disappearance of the humid conditions marked by coal layers and the extensive formation of calcareous paleosols, indicative of semi-arid conditions (this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. This Late Jurassic aridification affected most of Central Asia and was also identified in the West Siberian Basin (e.g., [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Le Heron | Evolution of Mesozoic fluvial systems along the SE flank of the West Siberian Basin, Russia[END_REF] and within the Turan domain where sedimentation partly consisted on thick evaporite units [START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF].

The Late Jurassic -Early Cretaceous transition was marked by a tectonic reactivation leading to localized relief building within the Tian Shan and coarse-grained proximal alluvial deposits surrounding the range (Fig. 16) (;[START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2012, 2013;[START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Meanwhile, the Yili and Bayanbulak basins were dominated by sediment by-pass and/or limited erosion.

Contemporaneous, limited relief building is also suggested in the Altai [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Yuan | Mesozoic-Tertiary exhumation history of the Altai Mountains, northern Xinjiang, China: new constraints from apatite fission track data[END_REF]. The Late Jurassic -Early Cretaceous transition was further characterized by the climax of the aridification trend which was prevailing since the early Late Jurassic. In the Junggar Basin, this peak in aridity has been associated to the deposition of alluvial fans together with large -scale aeolian dunes (Jolivet et al., 2017a).

2. AN EARLY -MIDDLE JURASSIC KINEMATIC FRAMEWORK DRIVEN BY

FAR-FIELD TECTONICS

The Jurassic tectonic and topographic evolution of the Tian Shan region is thought to be mostly controlled by compressive or transpressive events at continental scale (Allen et al., 1991;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF]Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Yang et al., 2015). Thus, Late Triassic-Early Jurassic evidences of deformation in the area are often related to the Qiangtang collision along the southern margin of Eurasia to the south, which ended at that time [START_REF] Kapp | Geological records of the Lhasa-Qiangtang and Indo-Asian collisions in the Nima area of central Tibet[END_REF][START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF]. However, no major collision episode has been reported along this Eurasian margin between the Qiangtang collision and the Early Cretaceous Lhasa collision [START_REF] Kapp | Geological records of the Lhasa-Qiangtang and Indo-Asian collisions in the Nima area of central Tibet[END_REF][START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF]. The absence of significant collision suggests that other kinematic events occurred during the Jurassic, leading to tectonic activity in the Tian Shan region. To the south, in the Tibet area, no major Jurassic geodynamic event has been described [START_REF] Roger | Timing of granite emplacement and cooling in the Songpan-Garzê fold belt (eastern Tibetan plateau) with tectonic implications[END_REF][START_REF] Roger | The tectonic evolution of the Songpan Garze (North Tibet) and adjacent areas from Proterozoic to Present: a synthesis[END_REF][START_REF] Reid | Structural evidence for the Permo-Triassic tectonic evolution of the Yidun arc, eastern Tibetan plateau[END_REF]. To the north-east, the timing of the final closure of the Mongol-Okhotsk Ocean remains poorly constrained. It is thought to occur during the Late Jurassic-Early Cretaceous time (e.g., [START_REF] Zorin | Geodynamics of the western part of the Mongolia-Okhotsk collisional belt, Trans-Baikal region (Russia) and Mongolia[END_REF][START_REF] Donskaya | Late Paleozoic-Mesozoic subduction-related magmatism at the southern margin of the Siberian continent and the 150 million-year history of the Mongol-Okhotsk Ocean[END_REF][START_REF] Daoudene | Late Jurassic-Early Cretaceous continental extension in northeast Asia-Relationships to plate kinematics[END_REF] and was probably not associated with strong compressive deformation (Fig. 17. A) but rather with distributed extension affecting a thin, abnormally warm crust [START_REF] Daoudene | Late Jurassic-Early Cretaceous continental extension in northeast Asia-Relationships to plate kinematics[END_REF]Jolivet et al., 2017b).

As mentioned above, in the Tian Shan region, east of the Talas Fergana/Karatau fault, the first order geometry of the Jurassic sediments preserved within the Tarim and Junggar basins is characterized by depocenters located along the Tian Shan Range (Fig. 17. B) (Lee, 1985;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Bian | Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. Moreover, recurrent periods

A C C E P T E D M A N U S C R I P T
of localized and limited Jurassic deformation associated with thrust faults have been reported

within the two basins (e.g., [START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Liu et al., 2006;Wang et al., 2012;[START_REF] Zhao | Intracontinental orogenic transition: Insights from structures of the eastern Junggar Basin between the Altay and Tianshan orogens[END_REF][START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF][START_REF] Ma | Kinematics of syn-tectonic unconformities and implications for the tectonic evolution of the Hala'alat Mountains at the northwestern margin of the Junggar Basin, Central Asian Orogenic Belt[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. These observations indicate that the Jurassic Junggar and Tarim basins were compressive basins and that the Tian Shan region was under compressional setting at that time (Allen et al., 1991;[START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]. Nonetheless, the Early-Middle Jurassic period was mainly characterized by the progressive planation of the Tian Shan relief established during the late Paleozoicearly Mesozoic [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Jolivet | Mesozoic and Cenozoic tectonic history of the Central Chinese Tian Shan: reactivated tectonic structures and active deformation[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF]. This implies that no major compressive tectonic event leading to an extensive relief building occurred in that area. The attested recurrent tectonic activity, together with the absence of a major relief build-up during this period, suggest strike-slip fault kinematics with limited vertical motion rather than true compressional tectonics. This idea is supported by seismic data interpretations that also indicate a Jurassic transpressional deformation in the Junggar Basin (Liu et al., 2006;[START_REF] Wang | Mesozoic faults in the NE Tarim (western China) and the implications on collisions in the southern Eurasian margin[END_REF][START_REF] Yu | Mesozoic reactivated transpressional structures and multi-stage tectonic deformation along the Hong-Che fault zone in the northwestern Junggar Basin, NW China[END_REF], which is potentially related to the Jurassic-Early Cretaceous rotation of the Junggar block [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yu | Mesozoic reactivated transpressional structures and multi-stage tectonic deformation along the Hong-Che fault zone in the northwestern Junggar Basin, NW China[END_REF]. Jurassic to Cretaceous strike-slip tectonics has also been described in the eastern part of the Tarim Basin [START_REF] Wang | Mesozoic faults in the NE Tarim (western China) and the implications on collisions in the southern Eurasian margin[END_REF] as well as extensional faults [START_REF] Yang | Middle-Late Jurassic tectonostratigraphic evolution of Central Asia, implications for the collision of the Karakoram-Lhasa Block with Asia[END_REF].

In the Tian Shan area, several NW-SE and E-W oriented lithospheric faults (e.g.,the Talas Fergana fault, the Nikolaev line, the North Tian Shan fault and numerous smaller ones) accommodated late Paleozoic block rotations [START_REF] Bazhenov | Permian paleomagnetism of the Tien Shan fold belt, Central Asia: post-collisional rotations and deformation[END_REF]Van Der Voo et al., 2006 and references therein). Similarly, we propose that these structures could have been geochronological studies (Rolland et al., 2013;Alexeiev et al., 2017).Along the southern edge of the Tarim Basin, geochronology data indicate that strike-slip motion of the Altyn Tagh fault occurred during Middle Jurassic times [START_REF] Dumitru | Uplift, exhumation, and deformation in the Chinese Tian Shan[END_REF][START_REF] Liu | Geochronology of the initiation and displacement of the Altyn Strike-Slip Fault, western China[END_REF]. However, the exact kinematic of these strike-slip motion as well as the direction of rotation of the blocks localized in the Tian Shan region is still unclear. Indeed, Jurassic clockwise or anticlockwise rotation of the Junggar Basin has been proposed in the literature (for example respectively in [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yu | Mesozoic reactivated transpressional structures and multi-stage tectonic deformation along the Hong-Che fault zone in the northwestern Junggar Basin, NW China[END_REF]. Similarly, both Jurassic dextral and sinistral motion along the Altyn Tagh fault have been suggested (Sobel et al., 1999;[START_REF] Liu | Geochronology of the initiation and displacement of the Altyn Strike-Slip Fault, western China[END_REF]. Finally, post early Permian sinistral strike-slip motion has been identified along the Nikolaev line in Kyrgyztan [START_REF] Bazhenov | Structural evolution of Central Asia to the north of Tibet: a synthesis of paleomagnetic and geological data[END_REF] but it is not clear if this kinematic prevailed during the Jurassic.

West of the Talas Fergana/Karatau fault,compressional events of regional significance occurred throughout the Caspian, Turan and south Kazakh domains during the Late Triassic leading to the inversion of numerous basins in this area [START_REF] Otto | Mesozoic-Cenozoic history of deformation and petroleum systems in sedimentary basins of Central Asia; implications of collisions on the Eurasian margin[END_REF][START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF].

Following this compressional phase, a widespread late Early to Middle Jurassic extension associated to back-arc development driven by the northward subduction of the Neo-Tethys oceans affected these regions (Zonenshain and Le Pichon 1986;Nikishin et al. 1998;[START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF][START_REF] Brunet | The South Caspian Basin: a review of its evolution from subsidence modelling[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF][START_REF] Robert | Structural evolution of the Kopeh Dagh fold-and-thrust belt (NE Iran) and interactions with the South Caspian Sea Basin and Amu Darya Basin[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]. This extension reactivated mainly NW-SE orientated Paleozoic structures as normal faults. In turn, these normal faults induced localized subsidence leading to the emplacement of elongated NW-SE depocenters in the Amu-Darya and Kopet Dagh basins (Fig. 17) (e.g., [START_REF] Robert | Structural evolution of the Kopeh Dagh fold-and-thrust belt (NE Iran) and interactions with the South Caspian Sea Basin and Amu Darya Basin[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]. Further east, Triassic -Middle Jurassic extension has also been reported in the western part of the Afghan -Tajik Basin [START_REF] Brookfield | The geology and petroleum potential of the North Afghan platform and adjacent areas (northern Afghanistan, with parts of southern Turkmenistan, Uzbekistan and Tajikistan)[END_REF].

Accordingly, the Talas Fergana/Karatau fault seems to be a major NW-SE structure To the north, the South Turgay Basin is characterized by a series of N to NW orientated grabens and half grabens, separated by basement highs and filled by up to 2.5 km of Lower to Middle Jurassic fluvio-lacustrine sediments (Moseley and Tsimmer, 2000;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Shi et al., 2016;Alexeiev et al., 2017). Within the central part of the Talas Fergana/Karatau fault, the Leontiev Graben is an elongate basin containing up to 1.5 km of Jurassic fluvial and lacustrine sediments (Sobel et al., 1999;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. Finally, at the south-eastern termination of the fault, the Yarkand-Fergana Basin consists of thick (c. a. 5 km) Lower to Middle Jurassic series of continental deposits (Sobel et al., 1999;[START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

Several studies propose that these basins formed in response to dextral strike-slip motion along the Talas Fergana/Karatau fault. This would induce the opening of the South Turgay Basin as a trailing imbricate fan and the opening of both the Leontiev and Yarkand-Fergana basins, either as dextral transtensional structures at right-stepping jogs in the fault system (e.g., [START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Alexeiev et al., 2017) or as pull-apart basins (Sobel et al., 1999). This kinematic model has been mainly based on geometrical analysis of seismic data conducted on the Turgay system (Alexeiev et al., 2017). These authors suggest that consequent Jurassic dextral strike-slip motion occurred along the Talas Fergana/Karatau fault, and its maximum offset was estimated by Alexeiev et al., (2017) to reach 70 km. On the other hand, [START_REF] Burtman | Faults of middle Asia[END_REF] considered Jurassic slip as insignificant along this fault in the Kyrgyztan region.

Finally, the driving mechanism leading to such dextral motion along the Talas Fergana/Karatau fault during the Early to Middle Jurassic period is yet to be fully understood.

Indeed, the precise onset age of formation of these basins is unclear. Rolland et al., 2013). The only coeval geodynamic event known in this region that could cause such dynamic is the Qiangtang collision which ended during the Late Triassic-Early Jurassic [START_REF] Kapp | Geological records of the Lhasa-Qiangtang and Indo-Asian collisions in the Nima area of central Tibet[END_REF]. Therefore we propose that the early Early Jurassic dextral motion along this fault could have been induced by far-field effects of the final stage of the Qiangtang collision. However, it is difficult to understand how such a far-field induced compressional regime could have led to the opening of the Yarkand-Fergana Basin. Indeed, Sobel et al. (1999) proposed the existence of a strike-slip fault system located in the Kunlun area during that same period, allowing the formation of a Jurassic transtensional basin encompassing both the Yarkand-Fergana and the western Tarim Jurassic deposits. However, seismic data obtained within the western margin of the Tarim Basin neither show the presence of a Jurassic depot-center nor the presence of any fault parallel to the Talas Fergana/Karatau one in this area (Fig. 17) [START_REF] Yang | Middle-Late Jurassic tectonostratigraphic evolution of Central Asia, implications for the collision of the Karakoram-Lhasa Block with Asia[END_REF]. This implies that both of these systems were disconnected from each other at that time. Moreover, opening of these basins continued during the late Early to Middle Jurassic (Sobel et al., 1999;Moseley et al., 2000;[START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]Alexeiev et al., 2017). During this period, no major collisional event has been identified

along the Eurasian margin implying that another kinematic event induced the tectonic activity observed along the Talas Fergana/Karatau fault. As mentioned previously, simultaneous widespread extension affected the whole Caspian-Turan domains to the west. We propose that this subduction related extension could also have affected the Talas Fergana/Karatau region leading to continuous opening of the South Turgay, Leontiev and Yarkand Fergana basins during the late Early-Middle Jurassic period.

Therefore, we propose that the early Early Jurassic evolution of the Tian Shan region was driven by the far-field effects of the Qiangtang collision final stage. However, recurrent tectonic activity persisted throughout the Tian Shan region during the Early -Middle Jurassic and such dynamic cannot be explained by this collision. The only regional geodynamic event

A C C E P T E D M A N U S C R I P T

affecting Central Asia during this period is the subduction of the Neotethys oceans which led to extension throughout the Caspian, Turan and south Kazakh domains (Zonenshain and Le Pichon 1986;Nikishin et al. 1998;[START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF][START_REF] Brunet | The South Caspian Basin: a review of its evolution from subsidence modelling[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF][START_REF] Robert | Structural evolution of the Kopeh Dagh fold-and-thrust belt (NE Iran) and interactions with the South Caspian Sea Basin and Amu Darya Basin[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]. We therefore assume that the extensional stress-field

3. A LATE MIDDLE TO EARLY LATE JURASSIC PERIOD OF RELATIVE TECTONIC QUIESCENCE

As explained above, the Jurassic topographic evolution of the Tian Shan Range was dominated by the progressive planation of a late Paleozoic to early Mesozoic relief. By Late Jurassic, almost all of the Tian Shan relief was thus flattened. Accordingly, even if a tectonic activity still occurred during the late Middleearly Late Jurassic, leading to the building of the Chemo uplift in the western part of the Junggar Basin for example [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF][START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF], it stayed moderate and localized on the major tectonic structures. Meanwhile, west of the Talas Fergana/Karatau fault, this period marked the onset of a post rift phase dominated by thermal subsidence following extension in the Caspian -Turan -Kazakh domains [START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF][START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]Mordvintev et al., 2017).

Thermal subsidence also occurred in the South Turgay and Fergana basins [START_REF] Clarke | Geology and possible uranium deposits of the Fergana region of Soviet Central Asia[END_REF]Moseley and Tsimmer, 2000;Alexeiev et al., 2017).

A C C E P T E D M A N U S C R I P T

4. A LATE JURASSIC -EARLY CRETACEOUS EVOLUTIONCONTROLLED BY FAR-FIELD COLLISION AND CLIMATE

The Late Jurassic -Early Cretaceous transition corresponds to a period of renewed transpression and localized uplift in the Tian Shan area (this study; [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF][START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2012, 2013;[START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF][START_REF] Tang | Mesozoic and Cenozoic uplift and exhumation of the Bogda Mountain, NW China: Evidence from apatite fission track analysis[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. Throughout the region, this period is marked by a sharp change in depositional environments with the emplacement of alluvial fan systems in the adjacent Junggar, Turfan, Tarim and Fergana basins. Along the Junggar Basin margins, the presence of angular unconformities at the base of conglomerate deposits indicates that tectonic movements occurred during this period [START_REF] Hendrix | Sedimentary record and climatic implications of recurrent deformation in the Tian Shan: evidence from Mesozoic strata of the north Tarim, south Dzungar, and Turpan basin, northwest China[END_REF][START_REF] Eberth | Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic-Cretaceous strata of the Junggar Basin, Xinjiang Autonomous R ion P op 's Republic of China[END_REF][START_REF] Vincent | Sedimentary record of Mesozoic intracontinental deformation in the eastern Junggar Basin, north-west China: response to orogeny at the Asian margin[END_REF]. Meanwhile, the Chemo-uplift reached its peak stage leading to the formation of a widespread paleorelief within the basin [START_REF] Lianhua | Provenance sediments and its exploration significance-A case from member 1 of Qingshuihe formation of Lower Cretaceous in Junggar Basin[END_REF][START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF][START_REF] Gao | Geomorphology and sedimentary sequence evolution during the buried stage of paleo-uplift in the Lower Cretaceous Qingshuihe Formation, Junggar Basin, northwestern China: Implications for reservoir lithofacies and hydrocarbon distribution[END_REF]. Similarly, in the Fergana Basin, the presence of an angular unconformity sealed by alluvial fan systems at the Jurassic-Cretaceous transition suggests that some tectonic movements occurred [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF].

Finally, Late Jurassic-Early Cretaceous compression has also been identified along the Talas Fergana/Karatau fault, since tectonic inversion and deformation have been described in the South Turgay (Yin et al., 2012), Leontiev (Allen et al., 2001) and Yarkand-Fergana basins [START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. However, if episodes of deformations have been reported in the Tian Shan region, numerous large-scale, pre-orogenic planation surfaces have been preserved

throughout the Tian Shan Range (e.g., [START_REF] Burbank | Partitioning of intermontane basins by thrust-related folding, Tien Shan, Kyrgyzstan[END_REF][START_REF] De Grave | The thermo-tectonic history of the Song-Kul plateau, Kyrgyz Tien Shan: constraints by apatite and titanite thermochronometry and zircon U/Pb dating[END_REF]Jolivet et al., 2010;[START_REF] Jolivet | Mesozoic tectonic and topographic evolution of Central Asia and Tibet: a preliminary synthesis[END_REF]. In the western Tian Shan, Upper Cretaceous strata overlying perfectly flat surfaces imply that no high relief existed in this region during the Early Cretaceous. Meanwhile, low temperature thermochronology data identified localized Late Jurassic -Early Cretaceous cooling event in the Kyrgyz Tian Shan Range suggesting only

A C C E P T E D M A N U S C R I P T

48 restricted relief building [START_REF] De Grave | Distant effects of India-Eurasia convergence and Mesozoic intracontinental deformation in Central Asia: Constraints from apatite fission-track thermochronology[END_REF], 2012, 2013;[START_REF] Glorie | Tectonic history of the Kyrgyz Sou h Ti n Sh n ( b shi-Iny ch k) su u zon : Th o of inh i d s uc u s du in d fo m ion-p op ion T c onics[END_REF][START_REF] Glorie | Exhuming the Meso-Cenozoic Kyrgyz Tienshan and Siberian Altai-Sayan: A review based on low-temperature thermochronology[END_REF][START_REF] De Pelsmaeker | Source-to-sink dynamics in the Kyrgyz Tien Shan from the Jurassic to the Paleogene: Insights from sedimentological and detrital zircon U-Pb analyses[END_REF]. However, despite, the lack of strong relief build up, this period is characterized by the emplacement of extensive alluvial fan systems in the basins surrounding the range (Fig. 15). Their development could be also strongly controlled by the contemporaneous climate aridification affecting this region (Jolivet at al., 2017a).

To the west of the Tian Shan area, a Late Jurassic -Early Cretaceous phase of tectonic deformation associated to the accretion of the Helmand Block also affected the Caspian -Turan -Kazakh domains and led to the inversion of the southern basins of Central Iran and Central Afghanistan [START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]. This deformation event also induced uplift within the Amu-Darya Basin [START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF] and up to the North Ustyurt Basin [START_REF] Otto | Mesozoic-Cenozoic history of deformation and petroleum systems in sedimentary basins of Central Asia; implications of collisions on the Eurasian margin[END_REF].

Based on the concordant ages of these events, we suggest that the Late Jurassic -Early

Cretaceous tectonic activity and the renewed localized relief building observed in the Tian Shan area was mainly related to the accretion of the Helmand Block to the south-west, and possibly to the onset of accretion of the Lhasa Block along the southwestern margin of Eurasia. This could also explain why stronger relief building occurred in the western part of the Tian Shan compared to its eastern part.

CONCLUSIONS:

Using both detailed field analysis conducted on the Chinese Tian Shan region and previously published data we reconstructed the Jurassic paleogeographical evolution of the Tian Shan region. See Table . 1 for the facies codes and descriptions. Pictures of facies respectively from: F1, Toutunhe Fm (Wusu section); F2, Xishanyao Fm (Wusu section); F3, Kalemake Fm (Yaha section); F4, F7 Qigu Fm, (Yaha and South Toutunhe sections); F5, Kalemake Fm (Yaha section); F6, Kezilenuer Fm (Yaha section) Fig. 4. Pictures illustrating the various Jurassic sedimentary facies of the Tian Shan region.

See Table . 1 for the facies codes and descriptions. Pictures of facies respectively from: F7, Qigu Fm (Yaha section), F8, Qigu Fm (South Toutunhe section) F9, respectively from Yengisar Fm (Yaha section), Toutunhe Fm (Nieleke section); F4, F10, Kalaza Fm (South Toutunhe section); F11, Kalaza Fm (Yaha section); F12, Kalaza Fm (Manas section); F13, Xishanyao Fm (Wusu section). Central Asia region. Regional Jurassic basins and main depocenters were derived from these studies; Lee (1985a, b); [START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF]Sobel et al., (1999); [START_REF] Fedorenko | Atlas of the lithologypaleogeographical, structural, palinspastic and geo-environmental maps of Central Eurasia. Center for geoinformation support of the military forces of Kazakhstan Republic[END_REF]; Alexeiev et al., (2017). Tectonic structures were compiled from [START_REF] Vnigni | Petroleum potential of Central Asia, 2 volumes[END_REF]; [START_REF] Thomas | Sedimentary record of late Paleozoic to Recent tectonism in central Asia-analysis of subsurface data from the Turan and south Kazak domains[END_REF]; [START_REF] Wang | Mesozoic faults in the NE Tarim (western China) and the implications on collisions in the southern Eurasian margin[END_REF]; [START_REF] Robert | Structural evolution of the Kopeh Dagh fold-and-thrust belt (NE Iran) and interactions with the South Caspian Sea Basin and Amu Darya Basin[END_REF]; [START_REF] Yang | Jurassic tectonostratigraphic evolution of the Junggar basin, NW China: A record of Mesozoic intraplate deformation in Central Asia[END_REF]; [START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]. The location and the geometry of the subduction zone were derived from [START_REF] Brunet | Late Palaeozoic and Mesozoic evolution of the Amu Darya Basin (Turkmenistan, Uzbekistan)[END_REF]

ACCEPTED MANUSCRIPT

  range together with the possible driving mechanisms. During the Early to early Middle Jurassic, the topographic evolution of the Tian Shan Range was dominated by progressive planation of late Paleozoic to early Mesozoic relief, locally interrupted by shortlived tectonic uplift. Throughout the region, contemporaneous sedimentation was characterized by alluvial to lacustrine strata deposited under humid conditions. During this period, recurrent limited deformation events associated with strike-slip and compressive tectonics occurred that cannot be explained by far field effect of the Qiangtang collision but could instead be associated to the coeval subduction-related extension affecting the Caspian -Turan domains. During the late Middle to early Late Jurassic, the planation of the Paleozoicearly Mesozoic Tian Shan Range then continued. A shift to more semi-arid conditions during

  accumulation + root traces + suspension fallout + overbank and waning flood currents + subaerial and subaqueous sheet and stream flows Distal alluvial plain environment with sandy alluvial deposits within floodplains and/or swamps

  ; Appendix B. 1). The transition with the Qigu Fm is progressive with deposits still characteristic of a lacustrine delta environment (LD) in the first 310 m of this formation. The next 90 m consist of distal alluvial plain deposits containing carbonate nodules indicative of semi-arid climate conditions (AP2a; Fig.6). The Qigu Fm then evolves up section towards lacustrine delta sediments (LD) to finally ends with proximal alluvial plain deposits (AP1). The boundary with the ~190 m-thick Kalaza Fm is sharp and marks a sharp change in depositional environments (Fig.6; Appendix B. 3). Indeed, the lower part of the Kalaza Fm is composed of a 50 -70 m-thick unit interpreted as erg deposits (EG) alternating with ~40 m thick units of alluvial fan sediments (AFa) (Appendix B. 4) (for more details seeJolivet et al., 2017a). This erg confirms the aridification trend already observed between the Toutunhe and Qigu formations. The basal part of the Lower Cretaceous Qingshuihe Fm shows a retrogradation towards a lake environment (LE1) (Fig.6; Appendix B. 5).

  The first 655 m of the logged Qigu Fm consists of interbedded red siltstones and sandstones interpreted as lacustrine delta deposits (LD) evolving in the last 145 m of the formation towards distal alluvial plain sediments containing carbonate nodules and desiccation cracks indicative of semi-arid conditions (AP2a) (Fig.7; Appendix C. 1, 2) . As in A C C E P T E D M A N U S C R I P T 21 the South Toutunhe section, the boundary between the upper Qigu Fm and the Kalaza Fm is sharp and corresponds to an abrupt change in depositional environments (Appendix C. 3).

  A C C E P T E D M A N U S C R I P Tretrogradational trend with depositional environments evolving from a proximal to a more distal alluvial plain (AP1, AP2) and finally to a lacustrine delta (LD).The Middle Jurassic Xishanyao Fm (~1705 m thick; Appendix D. 2) then comprises a poorly exposed basal series (570 m thick) showing a progradational trend from lacustrine delta (LD) to proximal alluvial plain (AP1) deposits. The topmost 1135 m of this formation show a retrogradational trend with environments evolving towards a distal alluvial plain (AP2) and a lacustrine delta (LD) associated with the presence of numerous coal beds indicative of rather humid climate conditions (Fig. 8; Appendix D. 3). At the top of the Middle Jurassic series, the sediments of the Toutunhe Fm are interpreted to represent a distal alluvial plain environment (AP2; Appendix D. 4). Following the Toutunhe Fm, a thick red beds series corresponds to the Upper Jurassic Qigu Fm (Appendix D. 5). The basal 315 m ofthis formation were interpreted as lacustrine delta deposits (LD) directly followed by ~65 m of distal alluvial plain sediments (AP2) (Fig.8). The rest of the Qigu Fm is characterized by a retrogradational trend with environments evolving from distal alluvial plain (AP2), to lacustrine delta (LD) and finally to a playa lake (LE1a). In the latter, desiccation cracks and carbonate nodules are indicative of semi-arid conditions. The transition with the Kalaza Fm is sharp with depositional environments passing from a playa lake (LE1a) to an alluvial fan (AFa) systems (Appendix D. 6, 7). The lower part of the Kalaza Fm corresponds to a rather proximal alluvial fan environment characterized by matrix-supported conglomerates associated with desiccation cracks and sparse root traces indicating arid/semi-arid conditions (AFa) (Fig.8). It passes up section into horizontal to sub-horizontal laminated clast-supported conglomerates characteristic of a more distal alluvial fan environment and deposited under semi-arid conditions. The transition with the basal part of the Lower Cretaceous Qingshuihe

  Even though the Early to early Middle Jurassic sedimentation in that area is mostly regarded as continental, Sha et al. (2011) and Pan et al. (2012) suggested h occu nc of b ckish w f un ("Waagenoperna") in the south Junggar Basin indicative of an intermittent connection with the Tethys Sea to the west. However, due to poor preservation, the "Waagenoperna" s fi u d nd d sc ib d f om h B d ow n Fm by Sh et al. (2011, 2016) and Pan et al. (2012) shows none of the characteristic generic features situated on the inner side of the shell (Simon Schneider, pers. com.). Moreover, it co-occurs with other bivalves which are clearly freshwater taxa, as stated by Sha et al. (2011) and Pan et A C C E P T E D M A N U S C R I P T 29 al. (2012) themselves.

  alluvial to lacustrine systems during the Middle Jurassic (this study;

  reactivated during the Jurassic accommodating the rotation of several blocks localized in the Tian Shan region. Such motion would favor the development of localized, small scale relief along these main faults. Early Jurassic reactivation along the Talas Fergana/Karatau fault has indeed been identified by kinematic analysis conducted on the south Turgay Basin and by A C C E P T E D M A N U S C R I P T

  separating the Tian Shan domain to the east, dominated by possible strike slip tectonics andA C C E P T E D M A N U S C R I P Tblock rotations and the Turan and southwest Kazakh domains to the west, dominated by extension. Along this fault, several basins formed during the Early-Middle Jurassic (Fig.17).

  fault was already active close to the Triassic -Jurassic transition in the Kyrgyz region (

  induced by the Neo-Tethys subduction also played a major role in driving the late Early to early Middle Jurassic tectonic and topographic evolution of the Tian Shan region. The farfield extension could have led to continuous opening of the basins previously formed along the Talas-Fergana Karatau fault while the rest of the Tian Shan was still possibly dominated by strike slip tectonics accommodated by the reactivation of the major NW-SE and E-W Paleozoic structures located within the range.

FollowingaFig. 1 .

 1 FIGURES CAPTIONS:

Fig. 2 .

 2 Fig. 2. Synthesis of the chronostratigraphic charts available for the Jurassic to Early

Fig. 3 .

 3 Fig. 3. Pictures illustrating the various Jurassic sedimentary facies of the Tian Shan region.

Fig. 5 .

 5 Fig. 5. Pictures illustrating the various Jurassic pedogenic and alteration features encountered

  Fig. 6 bis. Graphical caption presenting the various symbols used in Figs 6-12.

Fig. 7 .

 7 Fig. 7. Sedimentary log of the North Toutunhe section in the south Junggar Basin. Symbols as

Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13 Figure 14 Figure 15 Figure 16

 2345678910111213141516 Figure2

Figure 17

 17 Figure17

Table .

 .

	Facies Sandstone facies Lithology dm-to m-thick clast-	Sedimentary structures Massive conglomerates	Inferred depositional Hyperconcentrated
	M A N U S C R I P T processes a cm-to dm-thick coal beds Tabular beds containing Miscellaneous code F1 plant remains Peat accumulation F2 Several cm-to dm-thick white tuffaceous beds Massive Subaerial volcanic ash deposition F7 Stacked to isolated dm-to m-thick medium to coarse grained sandstones Tabular to slightly lenticular beds with sharp or low erosional basal boundaries. Trough cross-beddings, flat beddings underlined by rip-up clasts F11 supported conglomerates with erosive or sharp basal flows (Svendsen et al., 3D megaripples or with poorly-to moderately-boundaries and occasional 2003) alternating with planar beds of tractional sorted subangular to pebble imbrications 3D megaripple deposits currents deposits under subrounded pebbles to alternating with tabular or under sheet flows or subaerial or subaqueous boulders alternating with cm lenticular sandstones, stream flows (Miall, sheet flows and stream to m-thick medium to coarse structurless or with planar 1978) flows (Miall, 1978) grained sandstones laminations and trough and sometimes with current ripples at the top containing floating gravels cross-bedding Calcareous facies F3 a cm-to dm-thick siltstones interbedded with a cm-to dm-thick calcareous beds Massive to flat-laminated siltstone layers alternating with tabular calcareous beds with occasionally medium to strong bioturbation of the beds. Occasional a dm-to m-thick planar Horizontal to sub-Deposition from suspension fallout alternating with episodes of calcareous production Heterolithic facies F4 a m-to m-thick siltstones containing cm-to dm-thick fine-to medium-grained sandstones -Massive or flat laminated siltstones sometimes containing desiccation cracks or bioturbation -Tabular sandstone beds with sharp basal boundaries containing current ripples and sometimes bioturbation -Deposition from suspension fallout with some emergent events -Tractional current deposition (low energy flows; Miall 1978) with occasional periods of subaqueous biological reworking M A N U S C R I P T burrows F8 a m-to m-thick fine-grained to gravelly sandstones Slightly to strongly lenticular beds with erosional basal boundaries. Trough cross-stratifications or flat beddings (highlighted by gravels, coal and mud clasts) and current ripples; a dm-to a m-scale fining-up trends 3D megaripples, planar beds of tractional currents deposits under subaerial stream flows (Miall, 1978) F9 dm-to m-thick, stacked medium-grained to gravelly well-sorted, sandstones Tabular beds with sharp basal boundaries. Flat-beddings, trough and planar cross stratification, Tractional currents with planar beds, 2D and 3D megaripples under subaqueous sheet flows F12 couplets of mostly poorly-sorted conglomerates, angular to sub-angular gravels to boulder, and of poorly-to well-sorted sand horizontal bedded conglomerates and sandstones with erosive or sharp basal boundaries. Sometimes dm to m-thick M A N U S C R I P T channelled bed
	A C C E P T E D heterolithic facies composed of cm-to dm-thick siltstones interbedded with cm-to dm-thick fine to medium (rarely coarse) grained sandstone Flat laminated siltstone beds alternating with tabular sandstone beds containing current, climbing and/or oscillatory ripples; cm-scale soft sediment deformation structures, slightly to moderately bioturbated cm-to dm-thick siltstones alternating with cm-to dm-thick beds of fine-to coarse-grained sandstones Massive to flat-laminated siltstone beds alternating with sandstone beds either -Tabular containing flat laminations, occasional current and climbing ripples. Occasional plant fragments or -Lenticular and massive Conglomerate facies F5 F6 warts and ripples lamination with adhesion Irregular mm horizontal inverse climbing ripples. cross-laminations with A C C E P T E D sigmoidal beddings highlighted by gravels, coal and mud clasts and occasional current ripples; a dm-to dm scale dewatering structures and soft sediment deformation F10 a m-to m-thick fine-to coarse-grained sandstones, well-to moderately well-sorted m-to a dcm-high foreset composed of grainfalls and inverse climbing ripple. Horizontal laminations or very low angle mm-scale A C C E P T E D	Deposition from suspension fallout alternating with overbanks and waning floods, turbidity currents within a permanent water body (Mulder and Alexander, 2001). Deposition or reworking by waves and biological activity Deposition from suspension fallout 1978) stream flows (Miall, tractional currents under currents or from and Nielsen, 1986) overbanks, waning flood wet surface (Kocurek alternating with (Miall, 1978) and with some gravitational events Aeolian dune and traction deposition by high wind velocity or migration of wind ripples (Hunter 1977). Wind-blown sand to a
		with erosional basal
	boundaries with 1: Summary of the facies characteristics within the Chinese Jurassic Tian Shan and occasional rip-up mud
	their interpretation in terms of depositional processes clasts and plant fragments

  Table. 3. Fig. 15. Late Jurassic -Early Cretaceous paleogeography of the Tian Shan region atop of the present-day topography; AB: Aksai Basin; BB: Bayanbulak Basin; FB: Fergana Basin; IB: Issyk-Kul Basin; MB: Ming Kush Basin; NB: Naryn Basin; TB: Turfan Basin; YB: Yili Basin; YFB; Yarkand-Fergana Basin; ZB: Zahosu Basin. Fig. 16. Synthetic chart of the Tian Shan region: stratigraphic record, thermochronology (Thermo.), topography, climate and geodynamic events. Fig. 17. A. Late Early to Middle Jurassic paleogeography of the Asian continent (modified from Jolivet, 2017c); EU, European Craton; CIB, GCB; Great Caucasian Basin; SCB, South Caspian Basin; Central Iran Blocks; LH, Lhasa Block; QI, Qiangtang Block; SG, Songpan-Garzê prism; Q, Qaidam Block; Mon, Mongolian Block; NC, North China Block; SC, South China Block; IND, Indochina Block; SIB, Sibumasu Block; WB, West Burma Block; TFF, Talas Fergana fault. B. Late Early to Middle Jurassic kinematic framework of the west

  . ST: South Turgay Basin; LT: Leontiev Basin; YF: Yarkand Fergana Basin; B: Bayanbulak Basin; T: Turfan Basin; TFF: Talas Fergana/Karatau fault; NTSF: North Tian Shan fault; ATF: Altyn Tagh fault; 1, Paleotethys suture; 2, Turkestan suture; 3, Jinsha suture; 4, Kunlun suture.

Allegre, C. O., Courtillot, V., Tapponnier, P., Hirn, A., Mattauer, M., Coulon, C., ... and Burg, J. P., 1984. Structure and evolution of the Himalaya-Tibet orogenic belt. Nature,307(5946) Associated facies assemblages and their interpretation in term of depositional environments as in Table . 3. Fig. 9. Sedimentary log of the Wusu section in the south Junggar Basin. Symbols as in Fig. 6.

Associated facies assemblages and their interpretation in term of depositional environments as in Table . 3. Fig. 10. Sedimentary log of the Nieleke section in the Yili Basin. Symbols as in Fig. 6.

Associated facies assemblages and their interpretation in term of depositional environments as in Table . 3. Associated facies assemblages and their interpretation in term of depositional environments as in Table . 3.