1 Introduction

The Gartnerkofel borehole is one of the most thoroughly studied and described Permo-Triassic sections in the world(summary in Holser et al.1989,1991).Although Klein(1991)included organic carbon contents in his more inclusive study of elements,the results of detailed organic carbon isotope studies across the PTr boundary in the core have only been reported in a brief abstract(Wolbach et al.1994).In view of the importance of such studies in other Permo-Triassic sections,this paper summarizes these analyses of the total Gartnerkofel organic carbon,organic carbon isotopes,together with carbonate carbon and oxygen isotopes from Magaritz and Holser(1991),compares them with the total organic carbon analyses of Klein(1991)on the same samples,and compares our Gartnerkofel carbon patterns to other Permo-Triassic Tethyan sections.

2 Geology

The Gartnerkofel core was drilled in 1986 near the western end of the Permian Tethys Sea in a shallow-water shelf area interpreted as a currently eastward facing carbonate ramp(Brandner et al.2009)(Figs.1,2).

卷积神经网络（CNN）试图通过具有多个处理层的计算模型对数据进行多层抽象，是一个由INPUT（输入层）输入图像，CONV（卷积层）对图像进行卷积，再经过RELU（激活函数）传给POOL（池化层）进行池化，最后通过FC（全连接层）将所有特征连接起来的网络 [13]。实质上是一个学习特征的过程，经过CNN学习到的特征具有较强的辨别性，背景部位的激活度基本很少，通过可视化可以看到提取到的特征忽视了背景干扰，只提取目标中关键的信息交由后续的分类器对其进行检测与分类。

高校为了推进工匠精神与思想政治教育两者相互融合、相互促进，就必须为大学生的社会实践提供基地的保障，为社会实践活动创造条件。保障工匠精神的实践锻炼长期稳定能够保证实践活动的系统化、经常化、制度化，有利于形成科学、规范的实践教育体系。对基地进行长期有效的运营，建立完善的系统的机制有利于避免“走马观花”“蜻蜓点水”式的实践结果，保证实践锻炼能够循序渐进、扎实稳定的开展，从而使工匠精神能被学生更好地接受与运用。

Over most of its outcrop,the Late Permian Bellerophon Formation consists of thick carbonate-sulphate succession deposited in marginal(sabkha)to shallow shelf marine conditions with the top～1 m(Bulla member)consisting of more normal marine highly fossiliferous dark bioclastic wackestone,packstone and interbedded thin marls limestone with calcareous algae,foraminifera,mollusks and brachiopods(Noé1987;Farabegoli et al.2007).A top erosional surface on the Bulla Member is sharply overlain by the Tesero member of the Werfen Formation,which consists of diverse micrite,microbialites and marls interbedded with oolitic,peloidal and bioclastic packstones(Farabegoli et al.2007).The Tesero member blankets the underlying diverse Bulla Member facies,and varies little and irregularly(between 3 and 5 m)across the entire area,though it is absent between Bulla and Gartnerkofel(Noé1987).

秦明月与边峰看到他手指的是一辆白色的本田雅阁轿车，已经落满灰尘。老常相对谨慎了许多，他说我记得车左后门有撞的痕迹，边说边跑过去，果然左侧驾驶室门有一块撞痕。老常很肯定地说：“我记得当时的纸箱就是从这辆车的后备箱搬下来的。”

Fig.1 Late Permian palaeogeography(courtesy Ron Blakey)with places cited

The previously proposed carbonate ramp interpretation of the Tesero oolite section(Brandner et al.2009)is incompatible with the limited thickness and facies variations shown in the sections,and with the juxtaposition of very different sections across Alpine thrusts,with large translations of tens of km,within the Dolomites(Doglioni 1987).Thusthe Tesero ooliteismissing in the San Antonio section though present in the thrust sheets on either side(Fig.2).Furthermore the ramp interpretation(as shown in Fig.2b)is arbitrarily based on arranging Tesero oolite sections and the burrowed datum on which they rest,in a line downstepping to the east:the thinning of the lowermost oolite from Tramin to Gartnerkofel(interrupted by the fault-enclosed San Antonio section)is typical of carbonate platforms like the Bahama Bank,where marginal oolite shoals thin and pass into pelletoidal finer sediments towards the interior of the platform(Harris et al.2015).A flat carbonate platform environment fits the lack of horizontal but marked vertical facies change(during sea level variations)far better,and was the interpretation shown by Noé(1987)in the first comprehensive study of the PTr boundary sections in the area(Fig.2c).

In Kashmir In the transitional beds equivalent to the lower Tesero Member,zigzags inδ13Corg values(from-27‰ to-23‰)(Algeo et al.2007)are due to values from the background clays(more negative)and bioclastic beds introduced from shallower water(less negative)(Fig.4).In China,both Meishan and Shangsi show similar negative shifts in δ13 Ccarb but the δ13 Corg shows somewhat divergent trends(Fig.5).The Meishan section is,however,very condensed with several erosion surfaces which juxtapose very different isotope values:missing sediments needs to be taken into account(Zheng et al.2013).

The biodiversity drops markedly at the Bulla/Tesero contact but Permian brachiopods and bivalves persist into the Tesero Member(Posenato 2009).The first appearance datum(FAD)of the conodont Hindeodus parvus which defines the base of the Triassic is at 6 m above the base of the Tesero Member at Gartnerkofel,but only 2 m above the base at Bulla(Schönlaub 1991)(Fig.2).

The main lithological change(the Late Permian Event Horizon,LPEH)from the Bulla to the Tesero Members thus does not co-incide with the main extinction,nor with the base of the Triassic as defined by H.parvus.The strata between the LPEH and the base of the Triassic are thus of great interest for interpreting environmental changes associated with the extinction.

1.2.2 化疗方法 甲组40例患者应用吉西他滨联合顺铂治疗，即给予患者静脉滴注1 000 mg/m2吉西他滨+25 mg/m2顺铂。

3 Materials and methods

One set of PTr samples were used for all Gartnerkofel geochemical analyses(Klein 1991).

3.1 Wolbach and Gilmour methods

δ34S values of pyrite reflect the relative abundance of pyrite that formed within the water-column(syngenetic)and within the sediments(diagenetic),with lower values generally reflecting an increase in syngenetic pyrite due to anoxic or euxinic waters.The Tesero Member of the Bulla PTr section contains two relative minima inδ34Svalues of sulfide around-30‰with increases in S concentrations and S/Corg ratios(Gorjan et al.2007).The values in these intervals reflect an anoxic or euxinic water-column in the Tesero Member(Gorjan et al.2007),and similar valuesare recorded at multiple locations after the LPEH(Shen et al.2016 and references therein).At Gartnerkofel,the sharp increase in Sconcentrations and low values ofδ34Sin the Mazzin Member suggests an additional anoxic or euxinic interval in the Early Triassic,extending the record of transient anoxic intervals from the Tesero Member of the Bulla section.

Fig.2 a Location of Gartnerkofel and other PTr sections in the Dolomites,southern Alps.b Reconstructed cross-section of the Early Triassic carbonate ramp at the end of Tesero oolite deposition(after Brandner et al.2009,Fig.8),with representative sections.Note that the only the Tramin,Tesero and Bulla sections are in the same tectonic unit,the other sections are across thrust faults,and actual thickness variation is nowhere greater than 5 m across a horizontal distance of over 130 km.c Thickness variation and persistence of Bulla and Tesero Oolite facies from west to east(from Noé1987).Source:Stratigraphic columns:Tramin:Brandner et al.(2012);Tesero:Posenato(2009);Bulla:Farabegoli and Tonidandel(2012),Posenato(2009);San Antonio;Brandner(1988);Kraus et al.(2013);Dierico:Buggisch and Noé(1986);Gartnerkofel:Holser et al.(1991)

3.2 Klein(1991)methods

The carbon content was analyzed on separate aliquots of the powdered samples.For determination of total carbon(Ctot)a 100 mg portion was weighed into a ceramic crucibleby electronic balance.With aglassspoon about 2 g of LECOCEL(a Sn-W alloy)and 1 g of steel(7 ppm C,14 ppm S)were added.The mixture was combusted in a furnaceat 1400 °C,using oxygen(＞ 99.5%pure)ascarrier gas.The evolved gas CO2 was measured in infrared cells by integrating its peaks.The system was calibrated with LECO calibration samples and with internal laboratory standard Bellerophon Dolomite A/1.

Acknowledgements We thank R.Schmitt for donating the samples and J.Gibson for making the Cisotope measurements.We appreciate the comments of Elke Schneebeli-Hermann on an earlier draft of the manuscript.

Each sample was analyzed two to four times.The relative standard deviations were＜1%for C.For determination of organic carbon(Corg),500 mg of powder were weighed into a porous filter crucible,leached three times with 8 mL 2 M HCl,rinsed ten times with deionized water,and filtered with a filtering flask.The crucibles were dried in an oven at 150°overnight.Measurements were carried out as for total C.Acid-soluble carbon(Ccarb)was calculated by difference.

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4 Results

患者是有丰富情感的生命个体，一部分患者由于害怕术中或术后的疼痛，精神高度紧张，焦虑；还有一部分患者，认为手术没有不疼的，疼痛是可以忍受的，而且认为止疼药对身体有损伤且可能成瘾，不想应用镇痛药。针对前者，要为患者创造舒缓的环境，让家属朋友一起参与进来，如果有类似手术经历的亲戚朋友协同讲解能起到更好的效果。针对后者，我们要理解患者及家属的心理，首先表示认同他们的这种表现，然后可使用医学视频等手段来对家属进行教育，让他们对疼痛产生正确的认识，意识到完善的疼痛管理利远远大于弊，可与患者家属一起对患者进行引导。让患者及家属感到医生是以诚恳、负责地为患者切实着想的态度在做镇痛管理。

A detailed carbon isotope curve across the Permian–Triassic boundary for the thoroughly studied Gartnerkofel coreshowsδ13Corg valuesgenerally becomemorenegative upwards in parallel with theδ13 Ccarb values showing that atmospheric and oceanic carbon dioxide controlled both.Several extremeδ13Corg excursions,expressed in the δ13Corg–δ13 Ccarb values are attributed to periodic input of land vegetation either by storms or tsunamis.The overall trend of both δ13Corg and δ13 Ccarb values follow the other studied sections in the Alps and both northern and southern edges of the NeoTethys Ocean.

Nevertheless,the trends are the same in both analyses and the total organic values are all low in any case(Table 1,Fig.3).

在研究过程中，经过多方调研得知入室盗窃案件在长春乃至于全国都有明显的时空特征。因此，本研究以发案具体时间、月份、案发行政区域三个要素为指标进行统计。

Our organic carbon isotopestudiesshow anegativebase shift of-24‰ to-28‰ in the upper Bellerophon Formation to-26‰ to-28‰ in the Tesero Member,which latter values persists into the earliest Triassic Mazzin Member,after which it decreases slightly to-26‰(Table 1,Fig.3).Superimposed on this are two sharp negative peaks of＞ -38‰ in the Latest Permian(at 286.33 and 252 m depth)and a broader negative peak of＞-31‰ (215.07–207.14 m depth)in the Early Triassic(Fig.3).The two negative peaks in the upper Bellerophon Formation are not recorded in Wolbach et al.(1994)as they did not plot the values below 242 m.

Theδ13Ccarb values show a gradual drop from the Bellerophon through the Tesero Member into the lower Mazzin Member,followed by subdued fluctuations(Fig.3).This is consistent with the general average worldwide drop of-2‰across the PTr boundary(Korte et al.2001).

Theδ18Ocarb values also show a gradual drop from the Bellerophon into the Tesero Member after which they remain fairly constant until some zigzags in the lower Mazzin Member at the same level as the organic carbon zigzag(Fig.3).Although these beds show both Early and Late dolomitization(Boeckelmann and Magaritz 1991),and the oxygen isotopes therefore unlikely to be primary,and though the Gartnerkofel values are whole rock values,the significant fluctuations suggest that the oxygen isotopes in the section have not been homogenized.Under meteoric diagenesis Phanerozouc carbonate rocksshow elevated Mn and decreasing Sr contents due to dissolution of primary carbonate and precipitation of carbonate cements(Brand and Veizer 1980):carbonate samples with Mn/Sr ratio of＜10 might still retain their primary isotopic signatures(Kaufman and Knoll 1995).All Gartnerkofel samples studied have Mn/Sr ratios of＜5(data of Klein 1991).

It isinteresting that thegeneral warming trend acrossthe Tesero Member is compatible with the warming across thePermian–Triassic boundary in China inferred from conodont apatite(Sun et al.2012).The calculated seawater temperatures for Gartnerkofel based on Sun et al.’s(2012)methods,but using bulkδ18Ocarb values,show a low of-10 °C in the Ostracod unit rising to+6 to+26 °C in the overlying units.The Ostracod unit temperatures are unreasonably low,but may be caused by variable salinities in this sabkha-type environment(Mette and Roozbahani 2012).The higher temperatures are not inconsistent with a modern tropical carbonate environment like the Persian Gulf,where the lagoons and the open ocean can reach 24–32 °C and the coastal sabkhas can occasionally dip as low as 0°C(Al-Farraj 2005;Warren 2006).

Table 1 Carbon,carbonate and organic carbon isotope,and su8lfur and sulfur isotope data for the Gartnerkofel core

Sample Depth(m)This paper Klein(1991)Pak and Holser(1991)Corg(ppm)δ13Corg(‰)Corg(ppm) δ13Ccarb(‰)Magaritz and Holser(1991) Klein(1991)δ18O(‰)δ13Corg–δ13Ccarb S(ppm) δ34S(‰)46 115.95 152 1150 1.25 -4.76 72 58 130.55 9 650 1.14 -5.47 19 67 143.26 197 -26.67 840 1.58 -3.62 -28.25 200 79 158.33 16 550 1.35 -3.83 65 89 171.33 689 -27.88 650 1.12 -4.20 -29.00 158 98 180.33 435 -25.46 2700 0.31 -4.89 -25.77 75 376 -25.90 -25.90 110 184.43 82 -26.21 730 -0.79 -4.59 -25.42 162 116 185.51 145 -26.19 1080 -0.97 -4.31 -25.22 201 -19.5 120 186.15 65 -25.82 680 -0.83 -4.19 -24.99 550 125 186.93 392 -28.22 -0.44 -4.69 -27.78 200 391 -27.83 990 -27.83 135 189.23 472 -28.85 1150 0.48 -4.44 -29.33 230 450 -28.41 -28.41 148 193.00 485 -28.09 1350 -0.67 -2.25 -27.42 242 495 -28.13 -28.13 202.00 900 -26.00 900 0.58 -26.58 171 207.14 260 -32.00 1650 0.26 -7.21 -32.26 31 181 214.25 1040 -1.14 -3.82 222 182 215.07 1960 -32.10 1630 -1.41 -5.14 -30.69 495 2044 -31.82 -31.82 183 215.35 1920 -1.28 -3.68 6680 -23.3 184 215.70 1070 -0.93 -7.44 2285 185 216.30 2530 3540 186 216.62 4624 -28.67 1180 -1.12 -4.96 -27.55 670 187 219.70 700 -30.66 1490 -1.15 -4.44 -29.51 5120 724 -31.01 -31.01 188 220.10 1700 -29.90 1660 -1.39 -4.55 -28.51 5655 189 220.20 1650 -1.57 -4.46 6890 190 220.35 5500 -1.50 -6.51 16,700 -26.8 191 221.01 411 -27.68 970 -1.28 -3.99 -26.40 5440 -25.3 402 -28.38 -28.38 -25.0 192 222.08 3950 -1.14 -5.12 1230 -27.1 193 222.20 3540 -1.01 -4.98 33,100 -28.8 194 222.35 1490 -0.75 -4.26 182 194c 223.02 611 -27.88 -0.57 -4.44 -27.31 Sample Depth(m) This paper Klein(1991) Magaritz and Holser(1991) Klein(1991)Corg(ppm) δ13Corg(‰) Corg(ppm) δ13Ccarb(‰) δ18O(‰) δ13Corg–δ13Ccarb S(ppm)195 223.94 152 -26.20 650 -0.88 -4.10 -25.32 191.00 224.00 700 -27.10 -0.88 -26.22 196b 225.01 410 -26.41 0.33 -4.38 -26.74 198 226.00 163 -26.00 650 0.81 -4.25 -26.81 16.00 198c 227.02 299 1.08 -4.52 199b 228.04 202 -26.76 1.33 -4.49 -28.09-27.78 -27.78

Table 1 continued

Bold—data from Magaritz et al.(1992)

Sample Depth(m) This paper Klein(1991) Magaritz and Holser(1991) Klein(1991)Corg(ppm) δ13Corg(‰) Corg(ppm) δ13Ccarb(‰) δ18O(‰) δ13Corg–δ13Ccarb S(ppm)201 229.12 22 650 -4.06 18.00 204 229.92 236 840 1.10 -4.42 120.00 204c 230.60 332 -26.74 1.43 -4.63 -28.17 206 231.25 153 670 1.51 -4.82 148.00 208 231.72 105 -24.21 590 1.62 -4.79 -25.83 134.00 234.00 800 -25.20 1.74 -26.94 235.00 600 -24.30 1.64 -25.94 236.00 1500 -24.50 1.79 -26.29 240.00 600 -24.10 1.92 -26.02 241.00 600 -26.60 1.98 -28.58 218 241.89 442 -25.91 850 2.07 -3.85 -27.98 180.00 243.00 700 -24.10 1.86 -25.96 244.00 1000 -24.70 1.75 -26.45 223 251.00 592 -35.01 3070 2.27 -2.04 -37.28 183.00 590 -34.70 -34.70 252.00 800 -39.00 2.69 -41.69 254.00 1000 -24.50 2.12 -26.62 267.00 700 -23.90 2.83 -26.73 268.00 3400 -32.50 2.13 -34.63 277.00 900 -23.80 2.03 -25.83 247 277.98 26 2.52 0.35 140.00 255 286.33 176 -38.26 1300 2.74 -1.73 -41.00 58.00 268 296.40 15 650 3.32 -1.09 120.00 273 301.10 13 570 2.94 -1.65 70.00 306.00 800 -24.50 2.95 -27.45 310.00 700 -25.30 3.02 -28.32 280 311.34 167 650 3.19 -0.11 94.00 320.00 800 -23.10 2.66 -25.76 301 330.00 257 -26.35 3.28 -0.08 -29.63 75.00

Sulfur concentrations from Klein(1991)are generally very low and less than 0.02%.Only one interval between 215 and 222 m contains higher values generally greater than 0.50%and rangeup to amaximum of 3.31%and these are associated with early diagenetic framboidal pyrite developed under anoxic conditions(Wilkin et al.1996).The few availableδ34S values of pyrite from Pak and Holser(1991)range from-28.8‰ to-19.5‰.An up section trend of increasing δ34S values matches a decreasing trend in sulfur concentrations(Fig.3).

Fig.3 Late Permian to Early Triassic section of Gartnerkofel core(Holser et al.1991;Schönlaub 1991);organic carbon and organic carbon isotope plots(this study);organic carbon plots from data in Klein 1991);carbonate and oxygen isotope plots from data in Magaritz and Holser(1991);Sand Sisotope plots from data in Klein(1991),Pak and Holser(1991)(see Table 1).Note expanded scale from 232 to 222 m depth

To cover the PTr boundary adequately,bulk C residues were isolated from samples between 115.95 and 330 m depth in the core,using HCl and HF–HCl procedures of Wolbach and Anders(1989).Organic carbon wasseparated from any elemental carbon using extended acid dichromate oxidation(Wolbach and Anders 1989).Residues were combusted to CO2 for mass-spectrometric analysis,yielding isotopic data,and weights for organic carbon.Carbon isotopes were measured on a VG SWIRA 24 mass spectrometer using sealed-tube combustion.

5 Discussion and comparisons

Carbon isotope fluctuations in marine carbonates and marine plankton reflect the dissolved inorganic carbon reservoir in seawater.Organic carbon isotope fluctuations reflect the proportions contributed by marine and continental organic matter as well as by the contribution of green sulfur bacteria growing in anoxic conditions—negative trends in organic carbon isotope values have been used to infer anoxia(Berner 2005).

The strong fluctuations inδ13Corg values across the Permian–Triassic boundary in Alpine sections are readily attributable to variations in the proportions of marine versusterrestrial organic matter(Krauset al.2013).Therange of values ofδ13Corg reported for modern terrestrial higher plants(average-26.1‰),differs greatly from those for modern marine phytoplankton(average-17.7‰)(Wickman 1952;Craig 1953;Smith and Epstein 1971).Changes in δ13Corg values of up to 6.0‰,(from ～ -19‰ to-25‰)were measured across the Pleistocene–Holocene boundary in cores from the Gulf of Mexico abyssal plain,reflecting increased transport of terrestrial plant remains from re-established Holocene lowland forests to the Gulf basin(Newman et al.1973).In the Quaternary,therefore,increased land plant input is marked by more negative δ13Corg values.

In contrast to modern organics,Permian plant material has heavier carbon isotope values(δ13C=-24‰)compared with Permian plankton such as acritarchs(δ13C=-30‰)(Faure et al.1990;Strauss and Peters-Kottig 2003;Herrmann et al.2012).The difference from modern situations is because plants with C4 metabolism(all angiosperms)which have higherδ13Corg values between-8‰ and-15‰,did not evolve until the Cretaceous(O’Leary 1988).Kraus et al.(2013)noted that the Alpine PTr sectionsfrom near shoreto offshoreshowed the same organic carbon isotope trends but that the more offshore sections showed lighter,more negative values,consistent with greater plankton and lesser land plant input.Furthermore,their zigzag fluctuations inδ13Corg of up to 4‰in the Tesero Member are most plausibly caused by variations in land versus marine organic content,especially as theδ13Ccarb values do not change much.In contrast to Kraus et al.’s(2013)results,however,our main zigzag fluctuations occur lower down in the Bulla Formation,while their fluctuations in the Tesero member(admittedly based on much closer spaced samples)are not seen in our Tesero Member samples(Table 1,Fig.3).

The two very negativeδ13Corg peaks at 251/2(-35‰,-39‰)and 286 m(-38‰)depth at Gartnerkofel suggest marine incursions into the variable salinity Bellerophon sabkha environment.These extreme negativeδ13Corg values are,however,beyond the range of both mantlederived(δ13C=-5‰)and organic carbon,including sulphur bacteria(δ13C＜ -30‰)sources and require methane input(δ13C=-60‰)(Summons et al.1994;Higgins and Schrag 2006;Retallack and Krull 2006;Taipale et al.2015).Even the overlying Bulla and Werfen values need either almost pure marine organic sources or methane input—but the methane would need to be metabolized by organisms.One possibility is that the recently discovered ‘methane-eating’Methylobakter is responsible(Ettwig et al.2010).Since these use nitrate reduction in their metabolism,then they might be detected from nitrogen isotope studies(to be done).

Smallerδ13Corg fluctuations also occur above 222 m depth where pyrite,sulfur and,shortly above,carbon content increase,with a marked shift to lighter,more negative marineδ13Corg values(Holser et al.1989),consistent with the continuing Early Triassic marine transgression.The subsequent shift to heavier less negative values above 207 m suggests input of land plant material during the earliest Triassic which is recorded in other Alpine sections(Sephton et al.2002;Gorjan et al.2008).

The Val Badia section shows greatδ13Corg fluctuations during Late Permian Tesero Member times with a more detailed sampling than Gartnerkofel(Fig.4).In fact,all the PTr boundary section along both the southern and northern sides of the Neotethys and on the South China microcontinent show marked positive shiftsinδ13Corg valuesthough not necessarily at the same time if the correlations are accurate(Figs.4,5).If caused by greater land plant input,however,and if they are synchronous,then the positive shift is consistent with the destruction of land ecosystems and vegetation burning at this time,and with the marked negative shift inδ13 Ccarb at this time(Grasby et al.2011;Retallack 2013).

大数据和云计算方面，随着技术要求的提高，离线的单机模式的存储已经不能满足大数据和云计算的要求，GIS平台也已经由传统的单机版到web版然后发展到云环境版，比如知名的ESRI、SuperMap等公司的各种在线产品。在地质灾害监测中，也发展了基于WebGis、手机App和云计算的平台，将数据存储在网络中。蒋锐、宋焕斌等(2011)[16]提出一种基于SensorWeb的系统架构，联合多个矿山的局部监测网络，将监测信息汇集到管理部门，进行大数据的统一化管理。佘东、朱晓彦等(2013)[17]通过一种省级的云计算平台，提前或及时的预测地质灾害的发生，其本质上是一套WebGis+手机APP系统。

Furthermore,the Permian paleomagnetism of the Dolomites shows around 50°anticlockwise rotations of the southern Alps relative to central Europe during large post-Permian lateral movements and disruption of the Adria block(Muttoni et al.2013)and can thus not be compared to units now adjacent to it,like the Lombardy Verrucano to the west across the Judicaria fault(Gaetani 2010).

In all Tethyan sections noted here,the δ13Corg–δ13Ccarb values are greater in the shallower water sections like Gartnerkofel and Val Badia than in the deeper shelf sections at Guryul ravine,Shangsi and Meishan(Figs.4,5),which is in keeping with the decreasing continental input noted in the Alps(Kraus et al.2013).

If the zigzags in the organic carbon isotope curves between the LPEH and the base of the Triassic are due to different proportions of land-and marine-derived organic matter,then either a number of marine transgressions and regressions need to be considered(as they have in the past—e.g.Brandner et al.2009)or climatically-or eventcontrolled variations need to be considered.

Though rapid eustatic changes of sea-level occur in glacial times,there is no evidence of a Latest Permian glaciation and,in fact,the evidence is for rapid and significant ocean warming at the time(Sun et al.2012;Song et al.2014),which would raise sea-level by many metres due to thermal expansion since a 1°C rise in mean ocean temperature raises sea-level by 2 m(Southam and Hay 1981).Rising sea level during warming and bringing more marine conditions over the area during deposition of the Tesero Member would explain the gradually lighter trends in both δ13 Corg and δ13 Ccarb.Climate warming is thus a possible control—but a marine transgression in the Latest Permian does not explain the spasmodic input of landderived vegetation at thetime,nor theextremenegativeδ13 Corg values.

Input by backwash of land-derived material during storms,or even tsunamis,may explain some of the positive δ13Corg shiftsassociated with land vegetation input,even as far as the apparently isolated Bahamian-type Tesero oolite platform.Tsunami deposits have been identified in the Latest Permian in Kashmir,India(Brookfield et al.2013).Vast amounts of land-derived floating material were transported into and across the Pacific Ocean by the relatively small 2011 Japanese tsunami(Lebreton and Borrero 2013).The Tesero oolitic beds,with their hummocky cross-stratification and great extent(Brandner et al.2009)are also possible tsunamirather than simple storm deposits.

Total organic carbon and organic carbon isotopes of our study,together with the total organic carbon of Klein(1991),and carbonate carbon and oxygen isotope resultsof Magaritz and Holser(1991),plus the Sandδ34Sresults of Pak and Holser(1991)are shown on Table 1 and Fig.3.In our study,the brown color of all carbonaceous residues and rapid disappearance of residue aliquots on dichromate oxidation,together with their carbon content(～100%);indicate that the residues were composed entirely of organic carbon.The organic carbon content of the sediments was relatively low(＜2000 ppm)except at 216 m(＞ 5000 ppm),and at 215 and 268 m(＞ 2000 ppm)(Table 1,Fig.3).These high valuescorrespond with lower negativeδ13Corg values,which are in keeping with their inferred oceanic origin,as these samples were easily oxidized by dichromate—residual land-derived organic matter is much more difficult to destroy(Wolbach et al.1994).The total organic carbon results of Klein(1991)are divergent from ours and tend to be an order of magnitude higher(Table 1).The reasons for this are not entirely clear(we could not contact Peter Klein for comment),but could be due to:(a)sampling differences—unlikely,as we analyzed the same layers;(b)mineral acid differences—2 M HCl for Klein,9 M HCl followed by 15 M HF/1 M HCl for Wolbach,more aliphatic organic carbon would be destroyed by these methods—which would explain the lower Wolbach values;(c)destruction of silicates—by dissolving silicates,Wolbach freed up any carbon bound by the silicate crystal structure itself that carbon fraction would have been measured by Wolbach,but not by Klein—again this does not explain the lower Wolbach values;(d)oxidation—Wolbach made a concerted effort to destroy organics,then determine their isotopic values by difference whereas Klein measured organics directly,which might have missed silicate-encapsulated organics,but included any elemental carbon present with his Corg data and assumed it to be organic.

Fig.4 Comparison of Late Permian to Early Triassic organic carbon and carbonate Cisotopeplotsfor Gartnerkofel with variouslocalities along southern Tethyan margin(modified from Korte et al.2010)with additions and changes for Val Badia(Kraus et al.2013),Guryul(Baud et al.1996;Algeo et al.2007).Height between LPEH and base of the Triassic has been standardized for all sections

Fig.5 Comparison of Late Permian to Early Triassic organic carbon and carbonate Cisotopeplotsfor Gartnerkofel with variouslocalities along northern Tethyan margin and South China(modified from Korte et al.2010),with additions and changes for Djulfa(Kozur 2007;Ghaderi et al.2014),Shangsi(Wignall et al.1995;Jiang et al.2011;Riccardi et al.2007)Heping(Krull et al.2004).Height between LPEH and base of the Triassic has been standardized for all sections

6 Conclusions

瞭望台是森林防火工作的第一线，王宝生和他的同事两个人需要24小时不间断的瞭望，尤其是冬春时节持续干旱和夜里起大风的极端天气，风大的时候，炉子的烟根本抽不出去，会被大风压下来，满屋都是烟。王宝生索性就不生火取暖了，而是裹着大衣里三层，外三层的整夜瞭望。

一方面，工程建设对钢筋的需求量大，同一项工程对钢筋产品的型号、规格要求较多，同一批次所需的供货量多少不一，施工企业又希望能及时供货，这对于希望批量供货的钢铁企业来讲难以满足；另一方面，随着国家对产能过剩产业结构调整力度的加大，一些大型钢厂退出了建筑用钢的生产，而小钢厂又由于资金和技术限制，不愿意投入高强钢筋的研发。

Compliance with ethical standards

Conflict of interest All authors declare that they have no conflict of interest.

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