coversourcedb.igg.cas.cn/en/zjrck/200907/w...2798 district prediction of cholera risk in china based...

COVER The caterpillar fungus, Ophiocordyceps sinensis (best known as Cordyceps sinensis), infects ghost moth larvae in the Tibetan Plateau alpine ecosystems. The fungus then erupts from the dead insect head to produce sexual fruiting bodies. The fungus-insect complex, called “winter worm, summer grass” in Chinese, has been used for centuries as a highly-valued traditional Chinese medicine. The failure to artificially culture the sexual fruiting body and overharvesting due to the huge market demand have propelled the fungus towards extinction. The biology of this fungus largely remains unknown, including how it infects the insect hosts and the details of its sexual life cycle in the field. How the fungus survives the extreme cold winter in Tibetan Plateau is also a mystery. Genome analysis indicated that the caterpillar fungus is sexually self-fertile, but its sexual stage is only inducible by the appropriate, yet unknown, environmental factors. Relative to other insect fungal pathogens, the fungus has evolved an extremely large genome but with fewer genes for its specialized lifestyle. Fungal adaptation to extreme cold is putatively associated with mechanisms for increasing lipid accumulation and fatty acid unsaturation as well as enhanced function of antifreeze proteins (see the article by HU Xiao et al. on page 2846).

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Volume 58 Number 23 August 2013

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CONTENTS CONTENTSVolume 58 Number 23 August 2013

Progress of Projects Supported by NSFC

ARTICLE Geology2775 ChinesedesertsandsandfieldsinLastGlacialMaximumandHoloceneOptimum LU HuaYu, YI ShuangWen, XU ZhiWei, ZHOU YaLi, ZENG Lin, ZHU FangYing, FENG Han, DONG LiNa, ZHUO HaiXin, YU KaiFeng, MASON Joseph, WANG XiaoYong, CHEN YingYong, LU Qi, WU Bo, DONG ZhiBao, QU JianJun, WANG XunMing & GUO ZhengTang

REVIEW Geology2784 Earliestrecordofmegaphyllsandleafystructures,andtheirinitialdiversification HAO ShouGang & XUE JinZhuang

LETTER Atmospheric Science2794 Statistical estimations of atmospheric duct over the South China Sea and the Tropical Eastern Indian Ocean ZHAO XiaoFeng, WANG DongXiao, HUANG SiXun, HUANG Ke & CHEN Ju

ARTICLES PreventiveMedicine&Hygienics2798 District prediction of cholera risk in China based on environmental factors XU Min, CAO ChunXiang, WANG DuoChun, KAN Biao, JIA HuiCong, XU YunFei & LI XiaoWen

PreclinicalMedicine2805 Lidamycin inhibits tumor growth and pulmonary metastasis in murine breast carcinoma and shows synergy with

paclitaxel HU Lei, ZHANG ShengHua, SHAO RongGuang & ZHEN YongSu

Pharmacy2812 Cellularfluorescenthigh-throughputscreeningassaysoftheATP-gatedP2X7 receptor JIANG YaQin, YIN Qi & LI ShiYou

Cell Biology2820 Humanembryonicstemcells-derivedendothelialcelltherapyfacilitateskidneyregenerationbystimulatingrenal

resident stem cell proliferation in acute kidney injury JIA XiaoHua, LÜ He, LI Chen, FENG GuoWei, YAO XinPeng, MAO LiNa, KE TingYu, CHE YongZhe, XU Yong, LI ZongJin &

KONG DeLing

Bioinformatics2828 Bayesianoptimizationalgorithm-basedmethodssearchingforrisk/protectivefactors WEI Bin, PENG QinKe, CHEN Xiao & ZHAO Jing

Biochemistry&MolecularBiology2836 MicroRNA-142-3pisfrequentlyupregulatedincolorectalcancerandmaybeinvolvedintheregulationofcellproliferation ZHOU JiaLiang, JIANG Zhi, WANG ZhengWu, ZOU ShiTao, ZHANG YunXia, CAI Wei, WANG MingZhi, Xu Min, SHI DongTao &

CHEN WeiChang

Genetics2846 Genome survey uncovers the secrets of sex and lifestyle in caterpillar fungus HU Xiao, ZHANG YongJie, XIAO GuoHua, ZHENG Peng, XIA YongLiang, ZHANG XingYu, ST LEGER Raymond J, LIU XingZhong & WANG ChengShu

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CONTENTS CONTENTS

Developmental Biology2855 DEX1,aplasmamembrane-localizedprotein,functionsinmicrosporedevelopmentbyaffectingCalS5 expression in

Arabidopsis thaliana MA LiJuan, YANG ZhongNan & ZHANG Sen

2862 Derivation of androgenetic embryonic stem cells from m-carboxycinnamicacidbishydroxamide(CBHA)treatedandrogenetic embryos

SHUAI Ling, FENG ChunJing, ZHANG HaiJiang, GU Qi, JIA YunDan, WANG Liu, ZHAO Xiao-Yang, LIU ZhongHua & ZHOU Qi

Geology 2869 EmergedfossilcoralsonthecoastofnorthwesternHainanIsland,China:Implicationsformid-Holocenesealevelchange

and tectonic uplift YAO YanTao, ZHAN WenHuan, SUN JinLong & SUN Jie

2877 In situstableisotopicconstraintsondolomitizingfluidsforthehydrothermally-originatedsaddledolomitesatKeping,Tarim Basin

DONG ShaoFeng, CHEN DaiZhao, QING HaiRuo, JIANG MaoSheng & ZHOU XiQiang

Geography2883 Spatiotemporal variability of vegetation phenology with reference to altitude and climate in the subtropical mountain and

hill region, China QIU BingWen, ZHONG Ming, TANG ZhengHong & CHEN ChongCheng

MaterialsScience2893 Synthesis of antiferroelectric (Bi0.534Na0.5)0.94Ba0.06TiO3 ceramics with high phase transition temperature and broad

temperaturerangebyasolid-statereactionmethod LI XiaoJuan, XI ZengZhe, LONG Wei & FANG PinYang

2898 Clicking cyclophane to boron doped diamond surfaces WANG Mei

2903 BiocompatibilityofMg-Nd-Zn-Zralloywithrabbitblood WANG YongPing, OUYANG YuanMing, HE YaoHua, CHEN DaoYun, JIANG Yao, MAO Lin, NIU JiaLin, ZHANG Jian & YUAN GuangYin

HydraulicEngineering2909 Applicationandcomparisonofwinterwheatcanopyresistanceestimationmodelsbasedonthescaling-upofleaf

stomatal conductance WEI Zheng, LIU Yu, XU Di, CAI JiaBing & ZHANG BaoZhong

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Article

Geology August 2013 Vol.58 No.23: 28772882

doi: 10.1007/s11434-013-5801-7

In situ stable isotopic constraints on dolomitizing fluids for the hydrothermally-originated saddle dolomites at Keping, Tarim Basin

DONG ShaoFeng1,2, CHEN DaiZhao1*, QING HaiRuo3, JIANG MaoSheng1 & ZHOU XiQiang1,2

1 Key Laboratory of Petroleum Resources Research, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China; 2 Graduate University of Chinese Academy of Sciences, Beijing 100049, China; 3 Department of Geology, University of Regina, Regina SK, S4S0A2, Canada

Received January 9, 2013; accepted February 26, 2013; published online April 10, 2013

Detailed characterization of diagenetic fluid behaviour and evolution is commonly hindered by shortage of appropriate and eco-nomic methods to carry out in situ analysis in the tiny diagenetic mineral crystals. Using micromill sampling method, this study presents in situ stable isotopic data for the growth zones of saddle dolomite crystals in the hydrothermally-altered dolostones of Upper Cambrian (Furongian) at Keping, Tarim Basin, NW China. These data show minor and large variations in δ13C (−0.7‰ to −1.5‰ VPDB) and δ18O (−8.3‰ to −13.8‰ VPDB), respectively, from the cores to outer rims of the dolomite crystals and sug-gest that saddle dolomites precipitated from dolomitizing fluids with similar carbon sources but oscillatory temperatures during different formation stages. This scenario is confirmed by microthermometry of fluid inclusions within the growth zones of dolo-mite crystals. This study indicates that in situ isotope analysis could provide more detailed information related to the source and pathway of dolomitizing fluids, facilitating better characterization of dolomitizing fluids and processes.

Tarim Basin, Upper Cambrian, saddle dolomite, micromill sampling, in situ stable isotope analysis, fluid inclusion microthermometry, petrography

Citation: Dong S F, Chen D Z, Qing H R, et al. In situ stable isotopic constraints on dolomitizing fluids for the hydrothermally-originated saddle dolomites at Keping, Tarim Basin. Chin Sci Bull, 2013, 58: 28772882, doi: 10.1007/s11434-013-5801-7

Geochemical variations of diagenetic minerals are com-monly considered as the robust proxies to trace the fluid- rock interactions, sources and pathways of diagenetic fluids. Numerous researches had already successfully applied dif-ferent geochemical approaches to determine the types and pathways of dolomitizing fluids during dolomitization [1–8]. However, such efforts are commonly hindered by shortage of appropriate and affordable methods to extract in situ compositional information indicative of primary dolomitiz-ing fluids from the tiny diagenetic minerals. Therefore, sin-gle mineral crystals, even whole rock samples, are more often used for geochemical analysis; this would readily re-sult in mixing of geochemical signatures from different formation stages, limiting exact assessment for the diage-

netic fluid and its evolution. In recent decades, numerous efforts have been made to

develop reliable and affordable in situ isotope analysis methods with high spatial resolution. This greatly extends their applications in reconstruction of paleo-environment and paleofluid history [9–14]. Although laser ablation sam-pling can provide higher spatial resolution (~10’s μm) for in situ stable isotopic analysis, the uncertainties induced by composition-dependent isotope fractionation during laser ablation limit the routine application of this technique for carbonate rocks [9,11,14].

In order to better characterize the source and pathway of dolomitizing fluids, in situ stable isotope analysis, integrat-ed with cathodoluminescence (CL) microscopy and mi-crothermometry of fluid inclusions, were performed on the growth zones of saddle dolomite crystals from the hydro-

2878 Dong S F, et al. Chin Sci Bull August (2013) Vol.58 No.23

thermally-altered dolostones in the Lower Qiulitag Group of Upper Cambrian (or Furongian) well cropped out at Keping area, Tarim Basin, NW China.

1 Geological setting

The Keping section is situated along the southern part of Keping Uplift, northwestern flank of Tarim Basin, in the north of Keping County, southern Xinjiang, NW China (Figure 1). During the Early Paleozoic, the study area was located on a stable shallow marine carbonate platform on which very thick carbonate sediments up to 2000 m were deposited [15–17]. In the early Late Ordovician, carbonate deposition was terminated and gradually transferred into deepwater fine-grained siliciclastic deposition due to pro-gressive transgression [18].

During the Early Permian, intense volcanic activities took place extensively in Tarim block as a result of conver-gent subduction of Middle Tianshan arc to the north [19,20]. Near the end of Permian, the further amalgamation led to an extensive uplift and subsequent long-term subaerial expo-sure and erosion of Tarim block. As a result, the Mesozoic sequences were mostly absent or missed along the north-

western flank of the basin although locally present [21,22]. Since the Cenozoic, higher positive relief along the north-western flank was reinforced due to the collision of Indian plate farther south and Asian plate, forming a series of NEE-striking, imbricated overthrust nappes, including the Keping Uplift along the northwestern flank of Tarim block [20,23]. On the contrary, the vast areas of plate interior were subject to an accelerating subsidence and plunged downwards to depths, forming the widespread negative re-lief of Tarim Basin surrounded by numerous uplifts (or mountains) as seen today [20,24].

2 Methods

Detailed outcrop investigations, descriptions and sampling upon the selected section at Keping County were firstly carried out. Then, detailed petrographic examinations were conducted on hand specimens and double-polished thin sec-tions with thickened rock slices (0.5–0.8 mm) under micro-scope. These thin sections were further examined under the CL microscope to check the growth zonation on a RELIOTRON III stage from RELION Industries with a 5–8 kV beam and a gun current intensity of about 300–500 μA.

Figure 1 Simplified geological map in the Bachu and Keping counties, Tarim Basin, NW China. Inset map showing the main tectonic units in Tarim Basin. Stratigraphic system: Z, Sinian (Neoproterozoic); Є, Cambrian; O, Ordovician; S, Silurian; D, Devonian; C, Carboniferous; P, Permian; Q, Quaternary; Note the location of studied area (within the dashed square).

Dong S F, et al. Chin Sci Bull August (2013) Vol.58 No.23 2879

When the well-developed growth zones are selected, the thin section was transferred to the stereomicroscope in-stalled with micromill system and CL image was transmit-ted to the video mixing board and superposed on the aimed crystal. Afterwards, about 10–50 μg of saddle dolomite powers within CL-defined crystal growth zones were ex-tracted under the microscope using a low speed micromill drill assembly. The drilled powders were collected on the micropipette tips that were held in place by suction from the vacuum pump [13].

Stable isotope analysis was performed with a Finnigan MAT-253 mass spectrometer equipped with a Kiel IV car-bonate preparation device. The powders of each valve were reacted with ~50 μL of 103% H3PO4 at 72°C for 10 min. The generated CO2-gases were measured for δ13C and δ18O values that are reported in per mille (‰) relative to the Vi-enna Peedee Belemnite (VPDB) standard. All the δ13C and δ18O values were normalized to NBS19. The precision is better than 0.15‰ for δ18O and 0.10‰ for δ13C [25].

In addition, Microthermometrical measurement of fluid inclusions was carried out using the double-polished thin sections. The analysis was performed on a Linkam THM600 heating-freezing stage that was calibrated using the Fluid synthetic standard. The accuracy of final melting tempera-

ture of ice (Tm) and homogenization temperature (Th) values is within 0.5 and 2.5oC, respectively. All the analyses were carried out at the Institute of Geology and Geophysics, Chinese Academy of Sciences.

3 Petrography of saddle dolomite cements

In the studied section, the host dolostone is light to dark grey in hand specimen and consists of medium- to coarsely crystalline, non-planar tightly-packed matrix dolomites, ranging from 100 µm to 2 mm. Saddle dolomite crystals mainly occur as cements in the porous strata within a small- scale fault zone in the Lower Qiulitag Group of Upper Cambrian (Figure 2(a)). Within the fault zone, the dolo-stones were commonly subject to more intense fracturing and brecciation (Figure 2(b)), so that many fractures/ fissures and voids/cavities were produced. They were par-tially or completely filled by the saddle dolomite crystals and later calcite crystals (Figure 2(c) and (d)).

The saddle dolomite cements appear as milky white or pink in hand specimen, ranging from 250 µm up to 4 mm in size, with scimitar-, or half-moon-like terminations, and extensively occur around breccias, and along the walls of

Figure 2 (a) Field photo showing the panoramic view of studied section near Keping County, NW Tarim Basin. Note the fault crosscuts the thick dolo-stone which is overlain by Lower Ordovician limestones. The white lines represent fractures/fissures. (b) Field photo showing intense brecciation of host dolostones along the fault. Note the fractures were nearly completely occluded by the milky white saddle dolomite cements. Scale in centimeter. (c) Photo-micrograph showing saddle dolomite cement with different growth zones lining the wall of fracture. The inset dashed box is the area of (d). Cc, calcite ce-ment; Sd, saddle dolomite cement; Matr-dol, matrix dolomite; P, relict porosity. cross-polarized light. (d) Photomicrograph of saddle dolomite cements under CL. Note the nonluminescent core, bright red inner zone and dull red outer zones.


fractures and/or vugs (Figure 2(b)). They commonly exhibit curved or lobate crystal shape and display undulose extinc-tion under cross-polarized light (Figure 2(c)). Under ca-thodoluminescence microscope, most saddle dolomite crys-tals display a broad non-luminescencent or dark red core surrounded by a thin bright red rim which is further fol-lowed by a non-luminescent or dull red zone in some crys-tals (Figure 2(d)). Therefore, the saddle dolomite crystals were formed through three generations (core, inner and out-er zones) of growth.

4 Results and discussion

The δ18O and δ13C values of different growth zones within saddle dolomite crystals vary from −13.8‰ to −8.3‰ VPDB and from −1.5‰ to −0.7‰ VPDB, respectively (Ta-ble 1). Of these, a large decrease in δ18O value by 3‰ to 5‰ is well revealed in the inner zones with respect to the cores to outer zones of crystals. By contrast, the δ13C values are less variable from crystal cores to the outer rims, alt-

hough they are slightly low in inner zones as well (Table 1; Figure 3(a)).

The large fluctuations of δ18O values among growth zones of saddle dolomite crystals (Figure 3(a)) suggest epi-sodic variations in temperature and/or composition of dol-omitizing fluids during their precipitation. In this case, the cores and outer zones could have precipitated in dolomitiz-ing fluids with a relatively low temperature, and the inner growth zones with the highest temperature. Microthermom-etry of fluid inclusions corroborates the temperature varia-tions in dolomitizing fluids when corresponding zones formed, as is relatively low (Th: 110 to 130°C) in the cores and outer rims, the highest (Th: 140 to 170°C) in inner zones (Table 2; Figure 3(b)). This scenario indicates the oxygen isotope fractionation was mainly controlled by temperature in view of the persistently high salinity of dolomitizing flu-ids (Table 2). These data further suggest that the saddle do-lomites were formed from high-temperature (or hydrother-mal) dolomitizing fluids in which the kinetic barrier for dolomite formation was removed. Under this condition, the magnesium saturation became the key factor controlling

Figure 3 (a) Cross-plot of δ18O and δ13C values in different growth zones of individual dolomite crystals. Note the apparent isotopic offsets in the inner zone. (b) Histogram showing variations in homogenization temperatures (Th) of fluid inclusions in different growth zones of saddle dolomites.

Table 1 In situ oxygen and carbon isotopic data of different growth zones of saddle dolomites and matrix dolomites at studied section

Sample Dolomite type δ13C (‰, VPDB) δ18O (‰, VPDB)

09kp-04-03 core, non-luminescent band −1.0 −8.7






09kp-04-03 inner zone, bright red band −1.5 −13.8






09kp-08-01 outer zone, faint dull red band −0.8 −9.2

09kp-08-05 outer zone, faint dull red band −0. 9 −10.5

09kp-04 matrix dolomite −1.1 −8.0

09kp-08 matrix dolomite −0.6 −8.1

Dong S F, et al. Chin Sci Bull August (2013) Vol.58 No.23 2881

Table 2 Fluid inclusion data of different growth zones of saddle dolomite cements at Keping County

Sample Mineral type No. of

inclusions

Th (°C) Tm (°C) Salinity (wt% NaCl eq.)

Min Max Mean Min Max Mean Min Max Mean

09kp-04 sd-crystal core 4 106.2 147.9 120.2 −23.0 −13.0 −16.8 16.9 24.3 19.8




sd-inner zone 10 147.1 165.4 154.2 −25.0 −10.2 −19.8 14.1 25.6 21.8

sd-outer zone 5 116.8 126.6 121.8 −22.9 −18.1 −21.2 21.0 24.3 23.1

dolomite precipitation [26,27]. On the other hand, the small variations of δ13C values among different growth zones (Figure 3(a)) suggest that the dolomitizing fluids were de-rived from similar carbon source in absence of organic input during dolomite precipitation. However, the lighter δ13C values in the inner zones may have contributed by more mantle-originated hydrothermal fluids, which could have provided more isotopically light carbon input.

The occurrence of saddle dolomites in the fault zone as cements or infills of fractures and associated vugs (Figure 2) indicates that their precipitation was structurally controlled. Under this condition, the fracture network system could have provided favourable conduits through which the deep-seated hydrothermal fluids from the underlying strata were readily channelled and migrated upwards. Regional stratigraphic data indicate there are thick dolostones (sever-al 100s’ to ~1000 m thick) lie below the studied interval [18,21]. As the fluids migrated along the conduits that pen-etrated these dolostones, their magnesium content would

increase and reach a level supersaturated with dolomite through progressive hydrothermal fluid dissolution of the host dolostones. The relatively consistent δ13C values that are similar to those of host dolostones (Table 1) are likely a reflection of such a scenario (Figure 4). The tectonic evolu-tion of Keping Uplift suggests that it was subject to a sig-nificant elevation and possibly an exhumation in Mesozoic [21,22], as evidenced by widespread absence of Mesozoic sediments (Figure 1). Therefore, the structurally controlled hydrothermal activity must have occurred prior to extensive exhumation, which was likely associated with the wide-spread intense magmatism in Tarim block in the Early Per-mian [19,20,28–30]. Under this circumstance, the regional magmatic activity could have reinforced rock fracturing, thermal diffusion and hydrothermal fluids migration into the more porous dolostones during magmatic emplacement. If so, the temperature fluctuations during dolomite precipitation as stated above may be a reflection of the evolution of magma-tism, that is, relatively low at the start, the highest at

Figure 4 Conceptual model showing the structurally controlled hydrothermal dolomitization in the Upper Cambrian dolostones at studied section. The network fracture system could have worked as the principal conduits. Along these, the deeply-derived fluids were channelled and migrated upward and later-ally into the host dolostones, resulting in hydrothermal alteration (or recrystallization) of the antecedent matrix dolomites and precipitation of saddle dolo-mites from the hydrothermal fluids in fractures and/or cavities.


the acme and subsequent decrease at the waning stage of magmatism.

5 Conclusions

Saddle dolomites are commonly considered to be formed from hydrothermal fluids. This study used micromill sam-pling method, integrated with cathodoluminescence mi-croscopy and fluid inclusion microthermometry, to conduct in situ δ18O and δ13C analysis for the growth zones of saddle dolomite crystals from the structurally-controlled dolo-stones in the Upper Cambrian, Keping, Tarim Basin. These data demonstrate large δ18O fluctuations in the intracrystal growth zones of saddle dolomites. Saddle dolomites precip-itated in a heterothermal dolomitizing fluid probably linked to the different stages of magmatism emplacement within Tarim Block during the Permian. This study provides more accurate information of dolomitizing fluids and their evolu-tion, and improves our understanding for the mechanism of dolomitization.

Lab work was assisted with Wang Xu (in situ O and C isotope analysis) and Hu Fangfang (fluid inclusion microthermometry) from Institute of Geology and Geophysics, CAS. We thank two referees and the editor for their constructive comments which substantially improved the manuscript. This work was supported by SINOPEC (G5800-07-ZS-WX032), the Na-tional Key Scientific Special Program of China (2008ZX05008-003-002 and 2011ZX05008-003-10), the National Basic Research Program of Chi-na (2012CB214802), the State Key Laboratory of Oil/Gas Reservoir Ge-ology and Exploitation at CDUT (PL200801).

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Physics, Mechanics and Astronomy CHEN DongMin CHEN Hong GONG QiHuang LONG GuiLu

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Life Sciences MA KePing TIAN ZhiGang WU JiaRui WU WeiHua ZHAN QiMin

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DING DaJun FAN Jing FANG Jing GONG XinGao GUO GuangCan HOU MeiYing HU An

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ZHONG Yang ZHOU PingKun ZUO JianRu

Earth Sciences

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LI Yan LIU KamBiu LIU LiBo LIU XiaoDong LÜ HouYuan LU HuaYu LU QuanMing

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ZHU MaoYan

Materials and Engineering Sciences

CHEN XianHui CHEN XiaoDong CHENG HuiMing DAI LiMing DING Han DING JianDong GAO RuiPing

HE YaLing HU XiJun JIN HongGuang LEUNG Dennis Y C LI YanRong LI YongXiang LÜ ZhaoPing

LUO JianBin NAN CeWen NI JinRen SHI JianLin SU WanHua SUN HongBo SUN Jun

SUN YuanZhang SUNDELL Jan WANG RuZhu Wang XiaoLin WANG ZhongLin WEI BingBo XU ChunXiang

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LI CuiHua LI ShaoQian LIU Min LIU YuLiang LIU ZhiYong LU Jian LU ZuHong

MEI Hong NI Lionel M TAN Min WAN MingXi WANG FeiYue WANG HuaiMin WANG Jing

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ZHANG XueGong ZHAO JiZhong ZHU NingHua ZHU ShiHua ZHUANG YueTing

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