Lopingian Conodont Biostratigraphy and Age of Dalong Formation at Wujiachong Section, East Hubei Province
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摘要: 大隆组是华南地区乐平世一种重要的较深水沉积.为进一步探讨大隆组沉积的时空分布，选择对鄂东伍家冲剖面吴家坪组和大隆组重点进行了牙形石生物地层研究，此次研究共鉴定出牙形石1属5种，均为Clarkina，并由老到新识别出4个牙形石带：C.guangyuanensis带、C.transcaucasica带、C.orientalis带及C.wangi带.根据牙形石C.wangi的首现，将伍家冲剖面的吴家坪阶-长兴阶界线(Wuchiapingian-Changhsingian boundary，简称WCB)置于第18层底部.根据菊石Ophiceras的首现将伍家冲剖面的二叠系-三叠系界线(Permian-Triassic boundary，简称PTB)置于第20层顶部，仅高于WCB界线0.72 m.牙形石生物地层指示伍家冲剖面大隆组的主体为吴家坪期沉积产物.数个长兴期牙形石带的缺失和极短的长兴阶表明，该剖面长兴阶中上部可能因沉积间断存在缺失.
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关键词:
- 吴家坪阶-长兴阶界线 /
- Clarkina wangi /
- 二叠系-三叠系界线 /
- 古生物学
Abstract: The Dalong Formation is an important deep-water deposition during late Lopingian in South China. For better understanding of the spatial and temporal distribution of the Dalong Formation, detailed conodont biostratigraphic research is conducted from the Wujiaping Formation and Dalong Formation, at the Wujiachong section, East Hubei, South China. As a result, five species of genus Clarkina are recognized. Four conodont zones are established, and they are C. guangyuanensis, C. transcaucasica, C. orientalis and C. wangi zones, in ascending order. The Wuchiapingian-Changhsingian boundary (WCB) is placed at the base of bed 18 of the Wujiachong section based on the first occurrence of conodont C. wangi. The Permian-Triassic boundary (PTB) is placed at the top of bed 20 according to the first occurrence of ammonoid Ophiceras, only 0.72 m higher than WCB. Conodont biozones correlation suggests that the Dalong Formation of the Wujiachong section is mainly in age of Wuchiapingian. The absence of the several Changhsingian conodont zones and shorten Changhsingian deposition suggest that the middle and upper parts of Changhsingian of this section may be absent due to a hiatus. -
0. 引言
乐平世处于两次重要的生物灭绝事件，即瓜德鲁普世晚期生物灭绝事件及二叠纪-三叠纪(P-T)之交生物灭绝事件之间(金玉玕等，1995).在经历瓜德鲁普世末期大规模海退后，华南地区从吴家坪期开始缓慢海侵，至吴家坪阶-长兴阶界线(Wuchiapingian-Changhsingian boundary，WCB)时发生了轻微海退，随后长兴期又继续海侵(殷鸿福等，1994).研究乐平世地层对晚二叠世生物-环境变化过程及地质事件识别有着重要意义.如全球范围内，持续约30 Ma的二叠纪硅质岩沉积事件(The Permian Chert Event)在乐平世晚期也已结束(Beauchamp and Band, 2002).乐平统内部也存在一个重要界线，即吴家坪阶-长兴阶界线.碳同位素是进行地层对比及古环境研究的重要指标(Krull et al., 2004；Cao et al., 2010；安显银等，2020)，华南地区该界线附近，碳酸盐岩全岩无机碳同位素的负偏被广泛记录，且具有区域对比性(Shao et al., 2000；Jin et al., 2006；Shen et al., 2013；Wei et al., 2015；叶茜与江海水，2016).全球吴家坪阶-长兴阶界线层型剖面和点位(Global Stratotype Section and Point，简称GSSP)已经确立在我国浙江长兴煤山D剖面，以该剖面4a-2层底部牙形石Clarkina wangi的首现作为长兴阶底界的主要标志(Jin et al., 2006).
牙形石在地层研究中，尤其是我国华南等地的乐平世地层研究中应用广泛(如：梅仕龙等，1994；龚玉红，1996；Mei et al., 1998a, 1998b；王玥等，2004；金玉玕等，2007a；罗根明等，2008；杨宝忠等，2008；张克信等，2009；李俊等，2020).其中，吴家坪期牙形石曾报道于四川广元上寺(Yuan et al., 2019)、宣汉渡口、南江(梅仕龙等，1994)、重庆石柱(杨宝忠等，2008)、湘西北(田树刚，1993)及广西来宾地区(Mei et al., 1998a；王成源和吴健君，1998；金玉玕等，2007a)，被广泛用于区域地层对比.长兴期牙形石多报道于浅水相的长兴组灰岩中(王志浩和朱相水，2000；武桂春等，2003；王玥等，2004；袁东勋和沈树忠，2011；Yuan et al., 2014, 2015).由于较深水相可能更完整地记录地层信息，不易受到海平面变化影响，近年来，在广西东攀(罗根明等，2008)、贵州新民(Zhang et al., 2014)、湖南大窝岭(叶茜和江海水，2016)、鄂西五峰(Yang et al., 2019)等较深水剖面中也进行了牙形石生物地层研究，并可与浙江长兴煤山、四川广元上寺等研究程度较高的地区进行对比.
上述研究对乐平世牙形石带的区域对比及牙形石演化做出了重要贡献，而本文通过对鄂东伍家冲剖面吴家坪组至大隆组的牙形石生物地层的详细研究，既为华南地区乐平统生物地层，也为进一步探讨大隆组的时空分布提供独特的资料.
1. 区域地理位置及地质背景
伍家冲剖面位于湖北省阳新县王英镇北东方向约3 km处(29°49′13″N，114°50′56″E)(图 1)，距武汉市约100 km，距黄石市约50 km，易于到达.该剖面地层出露较为完整，从下到上分别为吴家坪组、大隆组和大冶组(图 2).其中，吴家坪组出露约11 m厚，岩性主要为灰白色厚层生物碎屑灰岩含硅质条带及团块；大隆组出露约2.4 m，岩性主要为灰黑色-黑色页岩、硅质泥岩，夹灰黄色粘土岩及硅质灰岩透镜体；大冶组底部出露约8.3 m，岩性主要为黄绿色薄层泥岩，偶夹灰绿-灰黄色火山灰，向上偶夹薄层灰岩.
图 1 湖北阳新伍家冲剖面交通位置Fig. 1. The location of the Wujiachong section, Yangxin County, Hubei Province伍家冲剖面地层分层及岩性描述如下：
描述
下三叠统大冶组(T1d)
30黄绿色薄层泥岩，顶部含双壳Claraia，该层富含黄铁矿. 0.60 m
29灰黄-黄绿色薄层泥岩，顶部含菊石Ophiceras、双壳Claraia. 1.20 m
28灰白色-灰绿色含火山灰粘土岩. 0.05 m
27黄绿色薄层泥岩，距顶部0.6 m处及0.3 m处含双壳Claraia. 1.90 m
26黄绿色薄层泥岩；顶部含菊石Ophiceras、双壳Claraia. 0.90 m
25黄绿色薄层泥岩，顶部含菊石Ophiceras. 0.75 m
24薄层黄绿色泥岩，顶部含双壳Claraia. 0.90 m
23灰白-灰黄色含火山灰粘土岩. 0.03 m
22黄绿色薄层泥岩，距顶部0.15 m含菊石Ophiceras . 1.30 m
21灰黄色含火山灰粘土岩. 0.01 m
20黄绿色薄层泥岩，顶部含菊石Ophiceras. 0.60 m
19灰白色-灰黄色含火山灰粘土岩. 0.04 m
-----------------平行不整合？-----------------
上二叠统大隆组(P3d)
18灰色薄层灰岩，顶面凹凸不平，似有剥蚀，采样WJ18-4.含牙形石C. orientalis、C. wangi. 0.08 m
17灰黑色页岩，侧向上伏有灰绿色含火山灰粘土岩. 0.08 m
16灰黄色含火山灰粘土岩. 0.02 m
15灰黑色页岩夹硅质泥岩. 0.11 m
14灰黑色薄层灰岩，采样WJ18-3.含牙形石C. orientalis. 0.08 m
13灰黑色页岩. 0.02 m
12灰黑色薄层灰岩，采样WJ18-2.含牙形石C. orientalis. 0.10 m
11灰黑色-黑色薄层硅质泥岩及页岩，上部含薄层硅灰岩夹层，采样WJ18-1.含牙形石C. orientalis. 2.35 m
10灰白色含火山灰粘土岩. 0.01 m
9灰黑色薄层硅质泥岩. 0.28 m
------------------平行不整合------------------
上二叠统吴家坪组(P3w)
8灰白色厚层生物碎屑灰岩，顶部凹凸不平，发育刀砍纹，似白云岩化. 1.40 m
7含硅质团块、硅质条带厚层灰岩，下部采样WYC-08，上部采样WYC-09.产牙形石C. liangshanensis、C. transcaucasica、C. guangyuanensis. 1.60 m
6硅质条带层0.10~0.22 cm
5灰白色生物碎屑灰岩，采样WYC-07.含牙形石C. guangyuanensis. 0.40 m
4灰白色厚层含硅质团块、硅质条带灰岩，下部采样WYC-05，上部采样WYC-06.含牙形石C. liangshanensis、C. guangyuanensis. 1.60 m
3灰白色厚层含硅质团块、硅质条带生物碎屑灰岩.顶部为20~40 cm厚硅质条带.下部采样WYC-03，上部采样WYC-04，含牙形石C. liangshanensis. 4.40 m
2灰白色厚层含硅质团块生物碎屑灰岩. 0.70 m
1厚层灰白色生物碎屑灰岩，底部含10 cm厚硅质团块，顶部也含硅质团块碎屑.含腕足，腹足类化石. 1.00 m
2. 方法与实验
在本次研究过程中，对伍家冲剖面吴家坪组-大冶组下部地层进行了细致的分层工作.在吴家坪组中采集牙形石样品10个，对大隆组的4层灰岩透镜体也分别采集了牙形石样品，每样重5~7 kg.将采集的岩石样品碎成约2~3 cm3小块，使用约10%浓度的醋酸溶液酸解，每隔2~3 d将底部不溶物质分离，分别以20目及160目样筛筛洗，去除余酸及杂质；烘干后使用密度配制为2.80 g/mL的LST重液(苑金玲等，2015)进一步分离牙形石，最后在双目体视镜下完成挑选.
3. 结果
本次研究共获得牙形石396枚(图 3~图 5)，鉴定出Clarkina属5个种：C. liangshanensis、C. guangyuanensis、C. transcaucasica、C. orientalis及C. wangi.在建立牙形石带时，以带特征分子的首现作为带的底界标志.本文将伍家冲剖面吴家坪期-长兴期牙形石序列由老至新划分为4个牙形石间隔带(interval zone)(图 6)，详述如下.
图 3 产自湖北阳新伍家冲剖面乐平统的牙形石(1)1~8. Clarkina liangshanensis (王志浩，1978)；1. WYC03-004，WYC-03；2. WYC09-015，WYC-09；3. WYC09-030，WYC-09；4. WYC09-012，WYC-09；5. WYC06-014，WYC-06；6. WYC09-021，WYC-09；7. WYC05-007，WYC-05；8. WYC05-008，WYC-05；9~12. Clarkina guangyuanensis (Dai and Zhang, 1989)；9. WYC05-011，WYC-04；10. WYC08-025，WYC-08；11. WYC07-024，WYC-07；12. WYC08-020，WYC-08；13~14. Clarkina transcaucasica Gullo and Kozur, 1992；13. WYC08-023，WYC-08；14. WYC08-016，WYC-08；15~20. Clarkina sp.；15. WYC09-005，WYC-09；16. WYC06-008，WYC-06；17. WYC09-026，WYC-09；18. WYC09-028，WYC-09；19. WYC09-029，WYC-09；20. WYC08-019，WYC-08. 线段比例尺为200 μm，a. 口视；b. 侧视Fig. 3. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 1)
图 4 产自湖北阳新伍家冲剖面乐平统的牙形石(2)1~14. Clarkina orientalis (Barskov and Koroleva, 1970)；1.WJ181-008，WJ18-1；2.WJ181-015，WJ18-1；3.WJ181-014，WJ18-1；4.WJ181-003，WJ18-1；5.WJ181-005，WJ18-1；6.WJ181-004，WJ18-1；7.WJ181-048，WJ18-1；8.WJ181-062，WJ18-1；9.WJ181-016，WJ18-1；10.WJ181-017，WJ18-1；11.WJ182-020，WJ18-2；12.WJ182-025，WJ18-2；13.WJ181-021，WJ18-2；14.WJ182-022，WJ18-2. 线段比例尺为200 μm，a. 口视；b. 侧视Fig. 4. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 2)
图 5 产自湖北阳新伍家冲剖面乐平统的牙形石(3)1~12. Clarkina orientalis (Barskov and Koroleva, 1970)；1.WJ182-026，WJ18-2；2.WJ182-028，WJ18-2；3.WJ182-030，WJ18-2；4.WJ182-029，WJ18-2；5.WJ182-031，WJ18-2；6.WJ182-036，WJ18-2；7.WJ183-041，WJ18-3；8.WJ183-049，WJ18-3；9.WJ184-050，WJ18-4；10.WJ184-054，WJ18-4；11.WJ184-065，WJ18-4；12.WJ184-020，WJ18-4；13~16. Clarkina wangi (张克信，1987)；13.WJ184-053，WJ18-4；14.WJ184-058，WJ18-4；15.WJ184-060，WJ18-4；16.WJ184-055，WJ18-4. 线段比例尺为200 μm，a. 口视；b. 侧视.所有标本保存在中国地质大学(武汉)地球科学学院地球生物学系Fig. 5. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 3)
图 6 湖北阳新伍家冲剖面二叠系-三叠系界线生物地层Fig. 6. Permian-Triassic biostratigraphy at the Wujiachong section, Yangxin County, Hubei ProvinceClarkina guangyuanensis带：此带分布于剖面第4~7层(图 6)，底界可能需要更多研究才能确定，以C. transcaucasica的首现为顶界，共生分子有C. liangshanensis.此带牙形石产出较稀少.本带的代表性分子见于华南地区上二叠统龙潭组及吴家坪组地层中(梅仕龙等，1994；王国庆和夏文臣，2004；金玉玕等，2007b)(图 7).本带可与四川宣汉渡口、南江(梅仕龙等，1994)、广元上寺(Yuan et al., 2019)、广西蓬莱滩(金玉玕等，2007b)、Shen and Mei(2010)综述中伊朗Zal剖面的同名带进行对比(图 7).本带归属层位为乐平统吴家坪阶上部.
图 7 全球重要剖面吴家坪阶-长兴阶界线牙形石带对比Fig. 7. Globally correlation of conodont zonation across the Wuchiapingian-Changhsingian boundaryClarkina transcaucasica带：此带分布于剖面第7~11层(图 6)，以C. transcaucasica的首现为底界，以C. orientalis的首现为顶界.本带可与四川广元上寺(Yuan et al., 2019)、广西蓬莱滩(金玉玕等，2007a)及伊朗地区Shen and Mei(2010)综述的同名带进行对比(图 7).在湖北地区，C. transcaucasica分子见于鄂西恩施天桥剖面(王国庆和夏文臣，2004)及宜昌五峰竹桥剖面(Yang et al., 2019)(图 7).王国庆和夏文臣(2004)在天桥剖面建立了C. guangyuanensis- C. transcaucasica带，这是由于C. guangyuanensis和C. transcaucasica在该剖面上的首现位置接近，但后者的延限更长，本带可与其进行对比.本带归属层位为乐平统吴家坪阶上部.
Clarkina orientalis带：此带出现于剖面第11~17层(图 6)，以C. orientalis的首现为底界，以C. wangi的首现为带顶.本带牙形石含量丰富.C. orientalis曾报导于我国华南浙江煤山剖面吴家坪阶顶部(王玥等，2004；张克信等，2009)，在湖北地区见于鄂西甘溪剖面(Nafi et al., 2006)及鄂西竹桥剖面(Yang et al., 2019)(图 7).本带可与湘西北地区(田树刚，1993)、四川宣汉渡口(梅仕龙等，1994)、广元上寺剖面(Yuan et al., 2019)、湖北甘溪剖面(Nafi et al., 2006)及Shen and Mei(2010)综述的伊朗Zal剖面的C. orientalis带进行对比(图 7).在华南地区，该带的主要共生分子为C. longicuspidata(张克信等，2009).在浙江长兴煤山D剖面，C. longicuspidata和C. orientalis分子的首现位置相近并一直延续到C. wangi分子的出现，张克信等(2009)将其定为C. longicuspidata-C. orientalis组合带，Yuan et al.(2014)对煤山D剖面的牙形石带进行了再研究，将其定为C. longicuspidata带，本带亦可与上述两带进行对比.
Clarkina wangi带：此带出现于剖面第18层(图 6)，以C. wangi的首现为底界，顶界未定.本带除产出较多的C. wangi分子外，还包括下伏地层上延的C. orientalis.C. wangi的首现代表了上二叠统长兴阶的开始(Jin et al., 2006).Mei and Henderson(2001)在浙江煤山剖面建立了C. wangi-C. subcarinata组合带，Mei et al.(2004)将C. wangi-C. subcarinata组合带下部占优势的C. wangi分子区分出来，自下而上划分为C. wangi带和C. subcarinata带.本带可与我国华南浙江煤山(张克信等，2009)、四川上寺(Yuan et al., 2019)、湖北甘溪(Nafi et al., 2006)以及伊朗(Shen and Mei, 2010)等地区的同名带进行对比(图 7).在浙江煤山地区该带之上的牙形石带为C. subcarinata带(Yuan et al., 2014)，但在本剖面C. wangi带之上未识别出牙形石带.本带层位归属为长兴阶下部.
4. 讨论
4.1 伍家冲剖面吴家坪阶-长兴阶界线
如上所述，乐平统长兴阶的底界由牙形石C. wangi的首现标定，其全球界线层型剖面和点位于浙江长兴煤山D剖面(Jin et al., 2006).在煤山D剖面，Clarkina wangi出现在长兴组第4a-2层，以C. subcarinata的出现为顶(Jin et al., 2006).在鄂东伍家冲剖面，C. wangi分子首现于第18层.因此，伍家冲剖面上吴家坪阶-长兴阶界线应被置于第18层底部.
4.2 伍家冲剖面二叠系-三叠系界线
虽然在伍家冲剖面没有获得下三叠统底界的标准化石牙形石分子Hindeodus parvus(Yin et al., 2001)，但在大冶组中发现了双壳化石Claraia(图 8)以及菊石化石Ophiceras(图 9).化石保存状况不甚理想，难以定种.双壳类化石Claraia是晚二叠世末期生物大灭绝后生态危机时期，具有较好全球广泛分布的灾难特征生物类群，在碎屑岩相和碎屑岩于碳酸盐岩混合相中大量出现是重要的三叠纪底部年代地层标志.双壳Claraia在鄂西峡口剖面的首现于早三叠世牙形石Isarcicella isarcica带底部(李慧等，2009).菊石Ophiceras常与Lytophiceras共生形成Ophiceras-Lytophiceras组合带(童金南等, 2004, 2005, 2019)，该带于煤山剖面上同样始于早三叠世底部牙形石Isarcicella isarcica带，其他剖面上亦一般高于二叠系-三叠系界限.在以湖南桑植、安徽巢湖、四川广元上寺、贵州克脚等为代表的深水相剖面中，Ophiceras均出现在早三叠世地层中(童金南等，2005；张宗言等，2009；蒋杨等，2018；Yuan et al., 2019).因此，华南地区菊石Ophiceras的首现代表着已经进入三叠系底部.综合地层和化石证据，我们将伍家冲剖面P-T界线暂置于第20层顶面，也即18层Clarkina wangi首现点0.72 m之上，伍家冲剖面不厚于72 cm的地层代表了长兴阶约1.8 Ma的时间跨度.
图 8 产自湖北阳新伍家冲剖面大冶组近底部的双壳化石双壳化石均为Claraia属.a，b. 24层；c. 26层；d，e. 27层；f. 29层. 1角硬币直径：19 mm；标尺最小刻度：1 mmFig. 8. Bivalves from the lowermost of the Daye Formation at the Wujiachong section of Yangxin, Hubei
图 9 产自湖北阳新伍家冲剖面大冶组近底部的菊石化石菊石化石均为Ophiceras属.a. 20层；b. 22层；c. 25层；e. 26层；d，f. 29层. 1角硬币直径：19 mm；标尺最小刻度：1 mmFig. 9. Ammonoids from the lowermost of the Daye Formation at the Wujiachong section of Yangxin, Hubei4.3 鄂东地区大隆组的时代
伍家冲剖面所在的鄂东地区在区域上属中扬子东部边缘，这一区域的大隆组是一套以灰黑色硅质泥岩、页岩为主，间夹有薄层含火山灰粘土岩及深灰色硅质灰岩透镜体的地层.在伍家冲剖面，吴家坪组灰岩-大隆组硅质泥岩的相变界线，第9层底部，亦即大隆组的底界位于C. transcaucasica带中，其时代对应为乐平世吴家坪晚期.而该剖面直至大隆组顶部第18层灰岩透镜体才出现长兴阶底部标志的牙形石C.wangi，表明在伍家冲剖面大隆组的时代大体仍处于吴家坪期.
在中扬子地区，He et al.(2013)在岩相古地理研究中将大隆组归为乐平世长兴期产物，但其地层时代划分未进行详细的生物地层讨论.牛志军等(2000)对鄂西地区大隆组进行了菊石生物地层研究，在大隆组下部建立了Konglingites带，其时代为吴家坪晚期.王国庆和夏文臣(2004)对鄂西天桥剖面进行牙形石生物地层研究，在吴家坪组顶部至大隆组建立了C. guangyuanensis-C. transcaucasica带、C.wangi-C. subcarinata带及C. changxingensis changxingensis-C.deflecta带，表明天桥剖面大隆组硅质岩的时代为吴家坪期中期-长兴期早期.在本研究剖面的邻区大冶，Lai et al.(1999)在西畈李剖面长兴阶长兴组中建立了C. changxingensis带，但在其剖面地层划分中，第2段为深灰色薄层硅质页岩，与伍家冲剖面大隆组岩性相近，该段硅质岩属于C. changxingensis-C. deflecta-C. subcarinata亚带，时代为长兴期中晚期.王国庆和夏文臣(2003)在邻区黄石二门剖面大隆组地层中建立了长兴期牙形石带：C. subcarinata-C.wangi带及C. changxingensis带.伍家冲剖面的长兴阶以第18层牙形石分子C.wangi的出现为底界，至第20层顶部早三叠世菊石Ophiceras的出现，仅厚0.72 m，相较于大冶西畈李剖面的4.61 m(C. changxingensis带)及黄石二门剖面长兴阶4.20 m的厚度存在较大差异.
鄂西竹桥剖面大隆组记录有C. orientalis-C. wangi-C. meishanensis带，相较Shen et al.(2010)所综述华南地区乐平统牙形石带序列，明显缺失了C. subcarinata带、C. changxingensis带以及C. yini带(Yang et al., 2019)，与此次研究结果类似.竹桥剖面大隆组24-25a层的岩性突变、24层顶面的不平整以及δ13Ccarb值的快速增加，表明这一剖面大隆组内可能存在较大沉积间断.在伍家冲剖面，第18层灰岩顶面凹凸不平(图 2c)，表明其上部可能发生了风化剥蚀，导致地层沉积的间断，这可能是伍家冲剖面长兴阶中上部牙形石带缺失的原因.综上，本剖面大隆组除第18层为长兴期外，主体为吴家坪期沉积.而鄂东区域如此相近的不同剖面的大隆组的时代差异有待进一步研究.
图 2 湖北阳新伍家冲剖面野外露头及部分剖面细节a.伍家冲剖面全景图；b.大隆组灰岩透镜体及吴家坪阶-长兴阶界线；c、d、e.第19、21、28层火山灰Fig. 2. Outcrops and some details of the Wujiachong section, Yangxin County, Hubei Province5. 结论
本文通过对湖北阳新伍家冲剖面进行的乐平世牙形石生物地层研究，在吴家坪组及大隆组中共识别建立了4个牙形石带，自下而上依次为C. guangyuanensis带、C. transcaucasica带、C. orientalis带及C. wangi带.根据牙形石C. wangi的首现位置，将伍家冲剖面的吴家坪阶-长兴阶界线置于第18层底.依据菊石Ophiceras的首现层位，暂将伍家冲剖面的二叠系-三叠系界线置于事件粘土层之上0.60 m的第20层顶面.湖北阳新伍家冲剖面大隆组的主体为吴家坪期沉积产物.
致谢: 牙形石照片在中国地质大学(武汉)生物地质与环境地质国家重点实验室完成.我们感谢王达成、杨正杰、张奇奇等在野外工作中提供的帮助.袁东勋博士和陈延龙博士在审稿中提出了宝贵意见；在此一并表示感谢！ -
图 1 湖北阳新伍家冲剖面交通位置
Fig. 1. The location of the Wujiachong section, Yangxin County, Hubei Province
图 3 产自湖北阳新伍家冲剖面乐平统的牙形石(1)
1~8. Clarkina liangshanensis (王志浩，1978)；1. WYC03-004，WYC-03；2. WYC09-015，WYC-09；3. WYC09-030，WYC-09；4. WYC09-012，WYC-09；5. WYC06-014，WYC-06；6. WYC09-021，WYC-09；7. WYC05-007，WYC-05；8. WYC05-008，WYC-05；9~12. Clarkina guangyuanensis (Dai and Zhang, 1989)；9. WYC05-011，WYC-04；10. WYC08-025，WYC-08；11. WYC07-024，WYC-07；12. WYC08-020，WYC-08；13~14. Clarkina transcaucasica Gullo and Kozur, 1992；13. WYC08-023，WYC-08；14. WYC08-016，WYC-08；15~20. Clarkina sp.；15. WYC09-005，WYC-09；16. WYC06-008，WYC-06；17. WYC09-026，WYC-09；18. WYC09-028，WYC-09；19. WYC09-029，WYC-09；20. WYC08-019，WYC-08. 线段比例尺为200 μm，a. 口视；b. 侧视
Fig. 3. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 1)
图 4 产自湖北阳新伍家冲剖面乐平统的牙形石(2)
1~14. Clarkina orientalis (Barskov and Koroleva, 1970)；1.WJ181-008，WJ18-1；2.WJ181-015，WJ18-1；3.WJ181-014，WJ18-1；4.WJ181-003，WJ18-1；5.WJ181-005，WJ18-1；6.WJ181-004，WJ18-1；7.WJ181-048，WJ18-1；8.WJ181-062，WJ18-1；9.WJ181-016，WJ18-1；10.WJ181-017，WJ18-1；11.WJ182-020，WJ18-2；12.WJ182-025，WJ18-2；13.WJ181-021，WJ18-2；14.WJ182-022，WJ18-2. 线段比例尺为200 μm，a. 口视；b. 侧视
Fig. 4. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 2)
图 5 产自湖北阳新伍家冲剖面乐平统的牙形石(3)
1~12. Clarkina orientalis (Barskov and Koroleva, 1970)；1.WJ182-026，WJ18-2；2.WJ182-028，WJ18-2；3.WJ182-030，WJ18-2；4.WJ182-029，WJ18-2；5.WJ182-031，WJ18-2；6.WJ182-036，WJ18-2；7.WJ183-041，WJ18-3；8.WJ183-049，WJ18-3；9.WJ184-050，WJ18-4；10.WJ184-054，WJ18-4；11.WJ184-065，WJ18-4；12.WJ184-020，WJ18-4；13~16. Clarkina wangi (张克信，1987)；13.WJ184-053，WJ18-4；14.WJ184-058，WJ18-4；15.WJ184-060，WJ18-4；16.WJ184-055，WJ18-4. 线段比例尺为200 μm，a. 口视；b. 侧视.所有标本保存在中国地质大学(武汉)地球科学学院地球生物学系
Fig. 5. Lopingian conodonts from the Wujiachong section of Yangxin, Hubei (part 3)
图 6 湖北阳新伍家冲剖面二叠系-三叠系界线生物地层
Fig. 6. Permian-Triassic biostratigraphy at the Wujiachong section, Yangxin County, Hubei Province
图 7 全球重要剖面吴家坪阶-长兴阶界线牙形石带对比
Fig. 7. Globally correlation of conodont zonation across the Wuchiapingian-Changhsingian boundary
图 8 产自湖北阳新伍家冲剖面大冶组近底部的双壳化石
双壳化石均为Claraia属.a，b. 24层；c. 26层；d，e. 27层；f. 29层. 1角硬币直径：19 mm；标尺最小刻度：1 mm
Fig. 8. Bivalves from the lowermost of the Daye Formation at the Wujiachong section of Yangxin, Hubei
图 9 产自湖北阳新伍家冲剖面大冶组近底部的菊石化石
菊石化石均为Ophiceras属.a. 20层；b. 22层；c. 25层；e. 26层；d，f. 29层. 1角硬币直径：19 mm；标尺最小刻度：1 mm
Fig. 9. Ammonoids from the lowermost of the Daye Formation at the Wujiachong section of Yangxin, Hubei
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