华南浮游相区早石炭世早期牙形刺分带和泥盆系、石炭系的分界

第 23 卷第2期古生物学报 Vol. 23, No. 2 

1984 年 3 月 ACTA PALAEONTOLOGICA SINICA Mar., 1984 

华南浮游相区早石炭世早期牙形刺分带 

和泥盆系、石炭系的分界 

王成源殷保安 

(中国科学院南京地质古生物研究所)(广西壮族自治区区域地质调查队) 

自1979 年第 9 届国际石炭纪会议提出泥 

盆系石炭系的分界,以牙形剌 praesulcata- 

sulcata 为生物地层标准后;国际泥盆系石炭系 

界线工作组,对泥盆系石炭系界线层型作了大 

量工作,但至今还没发现一个可以作为界线层 

型的剖面(Paproth,Streel,1982),因为欧洲的 

所有剖面都缺少 praesulcata-sulcata 的连续关 

系。因此,对中国泥盆系石炭系界线的研究, 

不仅对我国,而且在世界上也具有一定的意 

义,或许我们可以提供较为理想的泥盆系石炭 

系界线层型剖面。 

在第2届全国地层会议(1979)上,杨敬之、 

王成源依据当时的资料,对我国泥盆系石炭系 

的分界作了初步总结;根据对牙形刺的研究, 

将湖南贵州底栖相区的邵东段和革老河下亚 

段归属到泥盆系,将浮游相区泥盆系石炭系的 

分界置于菊石 Wucklumeria 带与 Gattendorfia 

带之间,即代化组与王佑组之间,并指出“需 

对王佑组与代化组之间的地层,进行逐寸的取 

样,以便进一步找到牙形刺 praesulcata 和 

sulcata 之间的界线,准确地确定两个组之间的 

关系。” 

全国地层会议之后,王成源、熊剑飞(1980 

年 1 月)去贵州省长顺县睦化系统地采集了牙形 

刺样品,经分析发现 sulcata 带至 sandbergi 带的 

牙形刺序列。1983 年 4 月,笔者又去睦化采样*, 

并去宜山拉利,南丹巴平、巴定等地测制剖面。 

这一工作,为我国浮游相区泥盆系石炭系界线的 

确定,以及我国早石炭世早期牙形刺序列的确 

立,提供了可靠的依据,也为国际泥盆系石炭系 

界线层型提供了中国的侯选型剖面。 

黔南、桂北浮游相区的 4 个泥盆系石炭系 

界线剖面,简述如下: 

1 贵州省长顺县睦化剖面位于贵州省长 

顺县睦化公社,距睦化村北约 500 米的公路边, 

距山坡上清朝石墓约 30 米。(样品号即层号, 

笔者是逐层无间隔取样的,插图 1) 

下石炭统 

未命名黑色结晶灰岩 

Mhd—Mha(厚度未测,约 5—6 米),黑色结 

晶灰岩,含牙形刺 Siphonodella cooperi, S. 

isosticha, S. obsoleta, S. quadruplicata, 

Polygnathus purus purus, P. p. sublanus 

王佑组 

Mh 1(厚 10 厘米)灰色薄层瘤状灰岩,夹黄色 

泥质灰岩,含牙形刺 Siphonodella crenulata, 

S. sandbergi, S. lobata, S. obsoleta, 

Pseudopolyanathus multidentatus 

Mh 2(厚 15 厘米)灰色致密灰岩,含牙形刺 

Siphonodella sandbergi, S. crenulata, S. 

lobata, Pseudopolygnathus multidentatus, 

Dinodus fragosus, D. leptus, Elictognathus 

laceratus, E. bilobatus 


Siphonodella sandbergi, S. duplicata 

Morphotype 2, Dinodus fragosus, S. leptus, 

三叶虫 Carbonocoryphe sp., Cyrtosymbole 

(Waribole) sp. 


Siphonodella duplicata Morphotype 2, S. 

cooperi Morphotype 2, Polygnathus comm- 

*参加野外工作的还有袁金良,赵元龙。

2 期王成源等:华南浮游相区早石炭世早期牙形刺分带和泥盆系、石炭系的分界 225 

unis communis, P. purus purus, 三叶虫 

Carbonocoryphe sp., Cyrtosymbole sp. 

Mh5—1(厚 8 厘米)灰色薄层灰岩,含牙形刺 


cooperi Morphotype 2, S. obsoleta, S. 

sulcata, Polygnathus longiposticus, P. purus 

purus, P. p. sublanus 


Siphonodella duplicata Morphotype 2, 

Polygnathus longiposticus, P. purus purus, P. 

p. sublanus, Bispathodus aculeatus aculeatus, 

Pseudopolygnathus dentileneatus 



sulcata, Polygnathus communis communis, P. 

purus purus, P, p. sublanus, 三叶虫 Carbo- 

nocoryphe sp., Cyrtosymbole sp. 


Siphonodella sulcata, S. duplicata Morpho- 

type1, S. praesulcata, Bispathodus aculeatus 

aculeatus, Polygnathus purus purus, P. p. 

sublanus 


Siphonodella praesulcata, S. sulcata, S, 

duplicata Morphotype 1, Polygnathus purus 

purus, P. p. sublanus. 三叶虫 Carbono- 

coryphe sp. 

Mh 9-1(厚 21 厘米)灰色致密灰岩,含牙形刺 

Siphonodella sulcata, S. praesuleata, 

Polygnathus communis communis, P. purus

226 古生物学报 23 卷 

purus, P. p. sublanus, Bispathodus aculeatus 

aculeatus 

Mh9-2(厚 9—12 厘米)薄的透镜状灰岩或瘤状 

灰岩,大致由 4 至 5 层薄层灰岩组成,含 

有较多的泥质,产牙形刺 Bispathodus 

aculeatus aculeatus, Polygnathus communis 

communis, P. purrs purus, P. p. sublanus, 

Siphonodella sulcata, 三叶虫 Carbonocor- 

yphe sp. 

Mh 10-1(Mh 10-1 和 Mh 10-2 为一透镜状灰 

岩,厚 9-30 厘米,分上、下两部份取样, 

上为 Mh10-1,下为 Mh10-2)灰色致密灰岩, 

含牙形刺 Siphonodella sulcata, Polygnat- 

hus purus purus, P. communis communis, 

Bispathodus aculeatus aculeatus 

Mh10-2 灰色致密灰岩,与 Mh10-1 一致, 

厚度变化较大,下部层面不平,含牙形刺 

Prolognathodus meischeneri, P. kockeli, P. 

collinsoni, P. kuehni (?), Volygnathus comm- 

unis communis. 

上泥盆统 

长顺页岩 * (厚 3-5 厘米) 黑色泥质页岩,风 

化后为黄色,含 Posidonia sp.和牙形刺 

Palmatolepis gracilis gracilis. 

代化组(上部) 

Mh 11(厚 12 厘米)灰色致密灰岩,上部层而 

不平 , 含牙形刺 Palmatolepis gracilis 

gracilis, P. g. sigmoidalis, P. g. expansa, 

Spathognathodus supremus, Siphonodella 

praesulcata, Pseudopolygnathus trigonicus, 

Bispathodus stabilis, Protognathodus meisc- 

heneri, Palmatolepis delicatula, Ozarkodina 

homoarcuata., 菊石 Parawucklumeria sp. 

Mh 12—Mh 13(厚 50 厘米)灰色致密灰岩,含 

牙形刺 Palmatolepis gracilis gracilis, P. g. 

sigmoidalis, P. g. expansa, Spathognathodus 

werneri, Pseudopolygnathus trigonicus, 

Palmatodella delicatula, Conchodontus 

ziegleri, gen. et sp. nov., “Spathognathodus” 

dentilobus sp. nov., S. supremus, Pelekys- 

gnathus sp., 菊石 Parawucklumeria sp. 

Mh 14(厚 26 厘米)薄层灰岩,含较多的泥质, 

产牙形刺 Palmatolepis gracilis gracilis,P. g. 

sigmoidalis, P. g. expansa, Siphonodella 

praesulcata, Pseudopolygnathus trigonicus, 

Bispathodus stabilis, Palmatodella delicatula, 

Spathognathodus supremus, “S” dentilobus. 

Mh 15—Mh 16(厚 45 厘米)灰色致密灰岩,产 


sismoidalis, P. g. expansa, Pseudopolygnat- 

hus trigonicus, Spathognathodus supremus, S. 

werneri, 三叶虫 Chaunoproetus sp., 

Mirabole sp., 菊石 Parawucklumeria sp. 

Mh 17(厚 18 厘米)灰色薄层状灰岩,产牙形 

刺 Palmatolepis gracilis gracilis, P. g. 

sigmoidalis, P. g. expansa, Pseudopolygnat- 

hus trigonicus, Palmatodella delicatula, 

Spathognathodus supreraus, Ozarkodina 

homoarcuata. 

Mh 18—Mh 22(厚 62 厘米)灰色薄层灰岩,产 


sigmoidalis, P. g. expansa, Pteudopolygna- 

thus trigonicus, Spathognathodus inornatus, 

Palmatodella delicatula, Tripodellus robu- 

stus, 三叶虫 Mirabole sp. 

Mh 23—Mh 24(厚度大于 2 米)灰色厚层灰岩, 

泥质灰岩,产牙形刺 Palmatolepis graeilis 


Bispathodus costatus, Pseudopolygnathus 

trigonicus, Spathognathodus werneri, Ozark- 

odina homoarcuata, 三叶虫 Phacops sp., 

Mirabole sp. 

2 广西南丹县六寨公社巴定剖面这一剖 

面的王佑组,由大约 2 米厚的瘤状泥质灰岩组 

成,含牙形刺 S.sulcata。王佑组之上为黑色 

* 长顺页岩系本文新命名的页岩,即代化组与王佑组 

之间的一层黑色页岩,含有较多的有机质,风化后 

变为黄色。厚度变化较大,在本文描述的剖面上, 

厚仅 3—5 公分,向北大约 l0 米处,则变为 20 多公 

分厚,在睦化附近其他剖面上,长顺页岩厚可达 30 

多公分。页岩中产有瓣鳃类 Posidonia sp.和少量牙 

形刺 Palmatole- pis gracilis gracilis。长顺页岩下伏 

岩层为代化组,含 P.g.gracilis,P.g.sigmoidalis, 

P.g.expansa,S. praesuleata,上覆岩层为王佑组, 

含 S.sulcata,P. kuehni.长顺页岩时代为晚泥盆 

世最晚期。标准地点在长顺县睦化公社北约 500 米 

公路边。长顺页岩在岩性与古生物特征上与西德的 

Hangenberg 页岩一致,仅厚度比西德的小得多。


泥岩,含菊石 Gattendorfia sp., Eocanites sp., 

Pseudorietites sp., Imitoceras sp.。代化组顶部 

以灰色薄层至中层泥质灰岩为特征,产丰富的 

菊石动物群 Wucklumeria sp., Parawucklumeria 

paradoxa,Kosmoclymenia undulata,Cymacly- 

menia sp., Cyrtoclymenia sp.。 

Bispathodus costatus 最早出现在代化组与 

王佑组分界线下 2 米的层位,与 Bispathodus 

stabilis, Palmatolepis gracilis gracilis, P. g. 

sigmoidalis, P. perlobata, P. minuts minuta, 

Polygnathus vogesi, Pseudopolygnathus trigon- 

icus 共生。在代化组还没发现 S.praesulcata, 

此剖面 sulcata 带的底界还不能确定,因为产 

S. sulcata 的层位之下,露头不好,没有取样。 

泥盆系石炭系间的界线在代化组与王佑组之 

间,即在 Wucklumeria-sulcata 带之间。 

3 广西南丹县巴平剖面位于南丹县芒场 

公社巴平东 1 公里处。王佑组由瘤状、小透镜 

体状灰岩组成,夹有泥岩,其上为黑色结晶灰 

岩。代化组的岩性特征与睦化、巴定的代化组 

一致。剖面情况如下: 

上覆岩层黑色泥岩(厚度未测) 

黑色结晶灰岩(未命名) 

层1黑色薄层至中层结晶灰岩,含硅质 

结核,厚 1 米,含牙形刺(ADM20—ADM21) 

Siphonodella crenulata, S. isosticha, S. obsole- 

ta, S. quadruplicata, Polygnathus longiposticus 

王佑组 

层2灰色扁豆状或小透镜体状灰岩,其 

间夹有黄色泥岩,厚 3.6 米。在此层上部约 1 

米范围内发现 sandbergi 带至 Lower crenulata 

带的化石。ADM19 Siphonodella cremdata,S. 

obsoleta, Dinodus fragosus; ADM 16-ADM 15 

Siphonodella cooperi, S. lobata, Pseudopo- 

lygnathus triangularis, P. pinnatus; ADM14- 

ADM11 Siphonodella lobata, S. cooperi, S. 

quadruplicata; ADM 10-ADM1 Siphonodella 

sandbergi, S. cooperi, S. lobata, S. qua- 

druplicata. Pseudopolygnathus triangularis。在 

第二层下部发现 sulcata 带至 sandbergi 带 

的化石 (C20-C28), C28 Siphonodella sandbe- 

rgi, S. cooperi.; C23 Siphonodella duplicata, S. 

cooperi; C22 Siphonodella sulcata, C20-1 

Siphonodella praesulcata, Polygnathus comm- 

unis communis, P. purus purus, P. p. sublanus 

代化组 

灰色泥质灰岩,产大量菊石、牙形刺以 

及三叶虫和腕足类。Wucklumeria sp., Parawu- 

cklumeria paradoxa, Palmatolepis gracilis 


Pseudo- polygmathus trigonicus, 在 C20-1 仅 

找到一个 S. praesulcata, 属 sulcata 带。 

4 广西宜山县拉利剖面位于广西宜山县 

拉利小峒,泥盆系石炭系界线上、下的地层, 

主要由瘤状灰岩和灰色灰岩组成。 

下石炭统王佑组 

LX5-1—Lx8 瘤状灰岩,夹有泥岩(厚 86 厘米), 

产菊石 Imitoceras sp. 牙形刺 Sipho- 

nodella duplicata Morphotype 1, S. 

sulcata, Bispathodus aculeatus aculeatus, 

Polygnathus purus purus, P. p. sublanus 

LX9—LX10 瘤状灰岩(厚 57 厘米),含牙形刺 

Siphonodella sulcata, S. praesulcata, Bi- 

spathodus aculeatus aculeatus, Polygnat- 

hus purus purus, P. p. sublanus 

LX11-1 小透镜体状灰岩,其间为泥岩(厚 10 

厘米),产菊石 Imitoceras subbilobatus, 

牙形刺 Siphonodella praesulcata, Polyg- 

nathus purus purus, P. p. sublanus 

上泥盆统代化组 

LX11-2—LX13 灰色致密灰岩(厚>122 厘米), 

含牙形刺 Palmatolepis gracilis gracilis, 

P. g. sigmoidalis, P. g. expansa, Pseudopo- 

lygnathus trigonicus。 

讨论与结论 

1 从上述4个剖面看插图 2,黔南、桂北 

浮游相区晚泥盆世晚期至早石炭世早期的地 

层,在岩性与化石方面是相似的,因此我们建 

议用相同的地层名称,即晚泥盆世晚期的地层 

称代化组,早石炭世早期的地层称王佑组。王 

佑组为扁豆状或小透镜体状灰岩,含较多的泥 

质,睦化的王佑组则含泥质较少。王佑组分布 

较广,由黔南至桂北(南丹、宜山、寨沙),均


有产出,王佑组在岩性上有变化,但与代化组 

在多数地区是易于区别的。王佑组底界为 

sulcata 带,覆于长顺页岩之上,上界可能是穿 

时的,最高可到 Lower crenulata 带。 

黔南、桂北代化组在岩性上是一致的,均 

产 Wucklumeria 菊石动物群。代化组的顶界应 

为长顺页岩。仅几公分厚的长顺页岩,暂不归 

入代化组,时代为泥盆纪。岩性与化石特征与 

西德的 Hangenberg 页岩一致。 

2泥盆系石炭系的分界 

在睦化剖面,泥盆系石炭系的分界,有以 

下 3 个问题是值得注意的: 

(1)长顺页岩的时代由于在代化组顶部 

(Mh11)存在大量的 Palmatolepis g.expansa, 

它的已知上限为中 costatus 带,但在 Mh11 及 

以下的层位中,还没找到中 costatus 带所特有 

的 P. g.gonioclymeniae 和 Bispathodus ultimus, 

仅在巴平的代化组上部找到 P. g. gonioclym- 

eniae (C18-2),因此还不能肯定长顺页岩,是属 

于中 costatus 带还是上 costatus 带,更不能确定 

它是上 costatus 带的下部、上部或代表整个上 

costatus 带 * ,但是可以肯定它归属泥盆系。 

(2)Mh10-2 的时代在样品 Mh10-1 中已 

出现 S. sulcata,无疑属早石炭世,Mh10-2 含 

典型的 Protognathodus 动物群。Protognathodus 

动物群代表一特殊的生物相,部份属 

praesulcata 带,缺少 P. kuehni;部分属 sulcata 

带,含有 P.kuehni。在 Mh10-2 中,仅发现 

一个可疑的 P.kuehni(?)(图版 III,图 13),如 

此标本果是 P.kuehni,则石炭系的底界在 

Mh10-2 之下,即王佑组与长顺页岩之间。如 

Mh 10-2 缺少 P. kuehni,属于 praesulcata 带, 

并在 Mh10-1 中发现可靠的 P.kuehni,泥盆系 

石炭系界线在 Mh 10-1 与 Mh10-2 之间,则睦 

化剖面可成为理想的界线层型剖面。 

(3)王佑组与长顺页岩之间的关系可能是 

连续的,但由于①在 Mh10-2 中,有可能存在 

P.kuehni,其下部缺少部份 Protognathodus 

动物群;②长顺页岩的时代不能精确的肯定; 

③王佑组与长顺页岩之间层面不平,页岩厚度 

变化大;④Mix 10 层厚度变化很快,相当 

Mhl0-2 的层位,在走向不到 2 米即消失;⑤长 

顺页岩本身是全球事件的重要标志,因此不能 

排除在王佑组和长顺页岩之间,存在一个小的 

间断的可能性。 

3 睦化剖面牙形刺分带 

(1)样品 Mh24-Mh11 相当 praesulcata 带, 

在这一层位中的每一样品,均有数以千计的 

Palmatolepis gracilis gracilis,P.g.sigmoidalis, 

P.g.expansa,Pseudopolygnathus trigonicus, 

在北美 praesulcata 最早出现在中 costatus 带。 

中 costatus 带的底是以 B.ultimus 出现为准, 

其顶界则以 P.g.goniodymeniae 消失为准 

(Ziegler,1962),这两个种在睦化剖面上均没 

发现,但是在这段地层中存在大量的 

P.g.expansa,它的已知上限是中 costatus 带, 

所以还不能排除这段地层属中 costatus 带的可 

能性。从睦化剖面看,praesulcata 可延至 Lower 

duplicata 带(Mh8)。 

(2)Mh10-2 相当于 Protognathodus 动物群, 

但由于没有发现可靠的 P.kuehni,还无法将 

这一动物群分为上、下两部份。Mh10-1 开始 

出现 S.sulcata,样品 Mh 10-1 与 Mh 10-2 是 

同一透镜状灰岩,厚 9—30 厘米,中间无岩性 

变化。 

* 最近笔者收到 Sandberg 博士 1983 年 12 月 8 日的来 

信。Sandberg 和 Ziegler 对晚泥盆世晚期的牙形刺带 

又作了重新划分。praesulcata 带分为 Lower , 

Middle 和 Upper 三部份。Lower praesulcata 带以 

S . praesulcata 出现为特征,含有 Pa. gr. 

gonioclymeniae,Ps.m.trigonicus,B.costatus, 

B.ultimus,Pa.gr.expansa,大致相当原来 Middle 

costatus 带的上部。Middle praesulcata 带下部以 

B.ultimus, B.costatus,Ps.m.trigonicus, 

Pa.gr.expansa 的绝灭为特征,大致相当 Upper 

costatus 带。Upper praesuleata 带以 Protognathodus 

kockeli 为特征,相当原来的 Lower Protognathodus 

Fauna 。从他们尚未发表的新资料看来, 

Pa.gr.expansa 的上限可到 Middle praesulcata 带 

的下部。长顺页岩的时代,大致相当于上 Middle 

praesulcata 带至 Upper prae tulcata 带。

2 期王成源等:华南浮游相区早石炭世早期牙形刺分带和泥盆系、石炭系的分界 229


(3)Lower duplicata 带始于 Mh 8,Lower 

duplicata 带与 Upper duplicata 带的分界,大致 

在样品 Mh6 与 Mh5 之间,在 Mh5 已出现 

Siphonodella obsoleta,S.duplicata Morphotype 

2。 

(4)sandbergi 带始于 Mh 3 ,Dinodus 

fragosus,D.leptus 在 Mh3 开始出现。 

(5) 样品 Mh2 与 Mha 中,有大量的 

S.sandbergi,但已开始有少数的 S.crenulata。 

由此,王佑组的最上部已属 Lower crenulata 

带。 

4 黔南、桂北牙形刺序列(由 praesulcata 

带至 Lower crenulata 带)的发现,为我国泥盆 

系石炭系界线的划分以及早石炭世地层的对 

比提供了较为精确的依据,华南浮游相区泥盆 

系石炭系的分界,可划在 praesulcata-sulcata 

带之间。 

nov. 

化石描述 

壳齿刺(新属)Conchodontus Wang 

et Yin gen.nov. 

模式种 Conchodontus ziegleri gen.et sp. 

12 个标本,保存好,可见一些个体发育阶 

段,新种 Conchodontus ziegleri 与 Palmatolepts 

gracilis gracilis,P. g. sigmoidalis,P. g. expansa, 

S. praesulcata 共生。 

齿台前后方圆或长圆,口面上有一矮的中 

齿脊和大的不规则的瘤齿。前端圆或有明显的 

“喙”状突伸,或者整个标本是伸长的。标本 

强烈拱曲,口面凸,中齿脊低从前端到后边缘, 

由不规则的瘤齿构成。中齿脊两侧瘤齿不规则 

或以一定形式排列。后边缘宽,光滑,反口面 

凹。凹窝深,在前方突伸内。反口面生长线清 

晰。 

齐格勒壳齿刺(新属、新种)Conchodontus 

ziegleri gen.et sp.nov. 

(图版 III,图 26—30) 

齿台亚圆形至长圆形,前方突伸,口面有 

瘤齿。齿台对称或不对称。中齿脊低,由前端 

延伸到后边缘,由不规则的瘤齿构成。在齿台 

前方瘤齿排列不规则,在后方呈放射状。后边 

缘宽,光滑,厚度薄。齿台厚度由后方到前端 

明显增厚。小的标本上,可见一中齿脊和中齿 

脊两侧的凹陷。在大的标本上,仅在中齿脊后 

方左侧有相对小的凹陷。 

前方突伸像腕足类的“喙”,而其反口面像 

“铰合面”,光滑。反口面凹,强烈拱曲,生长 

线同心状排列。凹窝在前端“喙”部内,被“铰 

合面”包围。反口面边缘在前方呈三角状,后 

方边缘薄。 

产地层位贵州省长顺县睦化;上泥盆统 

代化组,样品 Mh11,Mh13,praesulcata 带或 

中、上 costatus 带。 

壳齿剌(未定名新种)Concfiodontus 

sp. nov. 

(图版 III,图 31) 

仅一个标本,中齿脊较明显,仅口面边缘 

在前方呈半圆形。右侧边缘已断,其他特征同 

Conchodontus ziegleri gen.et sp.nov. 

产地层位广西南丹县巴平;上泥盆统代 

化组。praesulcata 带。 

齿叶“窄颚齿刺”(新种)“Spathognathodus” 

dentilobus sp.nov. 

(图版 II,图 11-13) 

“Spathognathodus” dentilobus 以特别大的 

外齿叶和不发育的内齿叶为特征,外齿叶上有 

一窄的中脊和 1—3 个细齿。基腔强烈不对称, 

接近齿片后方并仅限于齿叶下方。前齿片直而 

长,为后齿片长的 5 倍,口面单列细齿,前方 

有较高的细齿。由基腔至后端细齿高度减小。 

新种基腔位于后端与 Ozarkodina asymmetricus 

的基腔位置不同。外齿叶上有细齿不同于 

Amydrotaxis johnsoni 的 P 分子,内齿叶小以及 

基腔位置近后方也不同于 Ozarkodina 

transitans. 

产地层位贵州省长顺县睦化;上泥盆统 

代化组。praesulcata 带或中、上 costatus 带。


参考文献 

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15 号,l—152 页。 

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H. & Walliser, H. 0. (1974): The stratigraphical 

significance of the Protognathodus fauna from 

Stockum (Devonian-Carboniferous boundary, 

Rhenish Schiefergebirge). -Newsletter Stratigr. 3(4), 

263-276. 

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charts showing biostratigraphic zones and 

correlations based on conodonts from the Devonian 

and Mississippian rocks of the Upper Mississippi 

Valley. -Illinois Geol. Survey, Circ. 328, 1-32. 

Klapper, G. (1966): Upper Devonian and Lower 

Mississippian conodont zones in Montana, Wyoming, 

and South Dakota. -Univ. Kansas Paleontological 

contribution, Paper 3, 1-43, pls. 6. 

——, (1971): Patrognathus and Siphonodella (Conod- 

onta) from the Kinderhookian (Lower Mississippian) 

of western Kansas and southwestern Nebraska. 

-Kansas Geol. Survey Bull. 202 (3), 1-14, 2 pls. 

Nicoll, R. S. & Druce, E. C. (1979): Conodonts from the 

Fairfield Group, Canning Basin, Western Australia. 

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28 pls. 

Paproth, E. & Streel, M. (1982): Devonian- 

Carboniferous transitional beds of the northern 

“Rheinisches schiefergebirge”. -Guidebook of IUGS 

woking group on the Devonian-Carboniferous 

boundary. Belgium. 

Sandberg, C. A. (1979): Devonian and Lower 

Mississippian eonodont zonation of the Great Basin 

and Rocky Mountains, is Sandbergi, C. A., and Clark, 

D. L., eds., Conodont biostratigraphy of the Great 

Basin and Rocky Mountains-Brigham Young 

University Geology Studies, 26(3), 87-106. 

Sandborg, C. A. & Gutschick, R. C. (1979): Guide to 

conodont biostratigraphy of Upper Devonian and 

Mississippian rocks along the Wasatch Pront and 

Cordilleran Hingeline, Utah, in Sandberg, C. A., and 

Clark, D. L., eds., Conodent biostratigraphy of the 

Great Basin and Rocky Mountalns-Brlgham Young 

University Geology Studies, 26(3), 107-134. 

Sandberg, C. A. & Klapper, G. (1967) : Stratigraphy, age, 

and paleoteetonic significance of the Cottowood 

Canyon Member of the Madison Limestone in 

Wyoming and Montana. -U. S. Geol Survey Bull. 

1251-B: 1-70. 

Sandberg, C. A., Streel, M. & Scott, R. A. (1972): 

Comparison between conodont zonation and spore 

assemblages at the Devonian-Carboniferous 

boundary in the western and central United States 

and in Europe. -Congr. Internat. Stratigraphie et 

Geologic du Carbonifere, 7th, Krefeid, 1971, C. R. 1, 

179-203, 4 pls. 

Sandberg, C. A., Ziegler, W., Leuteritz, K. & Brill, S. M. 

(1978): Phylogeny, speciation, and zonation of 

Siphonodella (Conodonta, Upper Devonian and 

Lower Carboniferous). -Newsl. Stratigr., 7 (2), 

102-120. 

Wang, C. Y. & Ziegler, W. (1982): On the Devonian- 

Carboniferous boundary in South China based on 

conodonts. -Geologica et Palaeontologica, 16, 

151-162, 2 pls. 

[1983 年 11 月收到]


CONODONT ZONATIONS OF EARLY LOWER CARBONIFEROUS 

AND DEVONIAN-CARBONIFEROUS BOUNDARY 

IN PELAGIC FACIES, SOUTH CHINA 

Wang Cheng-yuan 

(Nanjing Institute of Geology and Palaeontology, Academia Sinica) 

Devonian-Carboniferous boundary is one 

of the focuses in the studies on stratigraphic 

boundaries of different periods. IUGS Devonian- 

Carboniferous Working Group has done much 

work on it since 9th International Congress on 

Carboniferous Stratigraphy and Geology in May 

1979, in which praesulcata-sulaata have been 

proposed as biostratigraphical boundary for 

Devonian-Carboniferous. But up to date none of 

sections in Europe provides a sufficiently 

detailed record to be proposed as a stratotype 

(Paproth and Streel, 1982). The absence of any 

section with an unambiguous praesulcata- 

sulcata junction illustrates this. Therefore, the 

detailed study of the Devonian-Carboniferous 

section of China is an urgent problem not only 

for China but also for the world. It is possible 

that China will provide an ideal potential 

stratotype section for Devonian-Carboniferous 

boundary. In the Second Stratigraphical 

Congress of All China (1979), Yang, J. Z. and 

Wang C. Y. summarized the work on the study of 

the Devonian- Carboniferous boundary in China, 

based mainly on conodonts and ammonoids. 

They have assigned the Shaodong member and 

the lower Gelaohe member in the benthic facies 

of Hunan and Guizhou to the Uppermost 

Devonian and drawn the Devonian- Carboni- 

ferous boundary of pelagic facies in South China 

between Wucklumeria-Gattendorfia, i.e. between 

the Daihua Formation and the Wangyou 

Formation. 

After the Second Stratigraphical 

Yin Bao-an 

(Regional Geological Surveying Team, Guangxi Province) 

Congress of All China, Wang, C. Y. and Xiong, 

Z.F. (Feb.1980) collected systematical conodont 

samples at the Muhua section of Changshun 

County and found the conodont sequence from 

the sulcata-Zone to the sandbergi-Zone. In early 

spring of 1983, the present authors collected 

again conodont samples at Muhua, Changshun 

County of Guizhou and at Lali, Yishan County, 

and Baping, Bading, Nandan County of Guangxi. 

As a result, the work has provided reliable 

material for the determination of the Devonian- 

Carboniferous boundary and the recognition of 

the Early Carboniferous conodont sequence in 

pelagic facies of South China, it also provides 

Chinese candidate section for Devonian- 

Carboniferous boundary stratotype. 

Stratigraphy 

Four sections across the Devonian- 

Carboniferous strata in southern Guizhou and 

northern Guangxi are briefly described as 

follows (Fig. 1, 2): 

1. The Muhua section, Changshun 

County, Guizhou Province. 

The section is situated at about 500 

meters N of Muhua village and exposed by road 

cut. The Uppermost Famennian to Lowermost 

Carboniferous rocks crop out. There is a Qin 

Dynasty stone tomb at the slope about 30 meters 

from the section. The lithological characters and 

fossils are as follows (Sample number=bed 

number): 

Lower Carboniferous


Unnamed black limestone: 

Sample Mhd-Mha (no measurement) 

Black crystalline limestone, containing 

conodonts: Siphonodella isosticha, S. cooperi, S. 

obsoleta, S. quadruplicata, Polygnathus purus 

purus, P. p. sublanus. 

The Wangyou Formation: 

Sample Mh1 (10 cm. in thickness) grey 

thin-bedded nodulose limestone with yellow 

argillaceous limestone, containing conodonts: 

Siphonodella sandbergi, S. crenulata, S. lobata, S. 

obsoleta, Pseudopolygnathus multidentatus. 

Sample Mh2 (15 cm.) grey dense 

limestone, containing conodonts: Siphonodella 

sandbergi, S. crenulata, S. lobata, Pseudopoly- 

gnathus multidentatus, Dinodus fragosus, D. 

leptus, Elictognathus laceratus, E. bilobatus. 



sandbergi, S. crenulata, S. lobata, Pseudopoly- 

gnathus multidentatus, Dinodus fragosus, D. 

leptus, Elictognathus laceratus, E. bilobatus. 


limestone, containing conodonts and trilobites: 

Siphonodella sandbergi, S. duplicata Morpho- 

type 2, Dinodus fragosus, D. leptus., Carbon- 

ocoryphe sp., Cyrtosymbole (Waribole) sp. 


limestone, bearing conodonts: Siphonodella 

duplicata Morphotype 2, S. cooperi Morphotype 

2, Polygnathus communis communis, P. purus 

purus, Carbonocoryphe sp., Cyrtosymbole sp. 

Sample Mh-5-1 (8 cm.). grey thin-bedded 


duplicata Morphotype 2, S. obsoleta, S. sulcata, 

Polygnathus longiposticus, P. purus purus, P. p. 

sublanus. 

Sample Mh5. (16 cm.) grey dense 

limestone, bearing conodonts: Siphonodella 

duplicata Morphtype 2, Polygnathus longip- 

osticus, P. purus purus, P. p. sublanus, 

Bispathodus aculeatus aculeatus, Pseudopolyg- 

nathus dentilineatus. 


limestone, bearing conodonts and trilobites: 

Siphonodella duplicata Morphotype 1, S. sulcata, 

Polygnathus communis communis, P. purus, P. p. 

sublanus., Carbonocoryphe sp.,Cyrtosymbole sp. 


limestone, yielding conodonts and trilobites: 

Siphonodella sulcata, S. duplicata Morphotype 1, 

S. praesulcata, Bispathodus aculeatus aculeatus, 

Polygnathus purus purus, P. p. sublanus. 


limestone, bearing conodonts and trilobites: 

Siphonodella praesulcata, S. sulcata, S. 

duplicata Morphotype 1, Polygnathus purus 

purus, P. p. sublanus., Carbonoeoryphe sp. 

Sample Mh9-1 (21 cm.) grey dense 


praesulcata, S. sulcata, Polygnathus purus purus, 

P. p. sublanus, Bispathodus aculeatus aculeatus. 

Sample Mh9-2 (9-12 cm.) thin lenticular 

limestone with marls, containing conodonts and 

trilobites: Siphonodella sulcata, Bispathodus 

aculeatus aculeatus, Polygnathus communis 

communis, P. purus purus, P. p. sublanus., 

Carbonocoryphe sp. 

Sample Mh10-1 and Mh10-2 are 

limestone lenses, 9-30 cm. think. We collected 

two samples, Mhl0-1 from the upper and 

Mh10-2 from the lower, grey dense limestone 

containing conodonts: Siphonodella sulcata, 

Polygnathus purus purus. P. p. sublanus, P. 

communis communis, Bispathodus aculeatus 

aculeatus. 

Sample Mh10-2 grey dense limestone, 

containing conodonts: Protognathodus meisck- 

eneri, Proto, kockeli, Proto. collinsoni, Proto. 

Kuehni (?), Polygnathus communis communis, 

Bispathodus aculeatus aeuleatus. 

Upper Devonian 

Changshun shale (3-5 cm.) (= Hangen- 

berg shale): black shale, weathering yellow, 

containing Posidonia sp. and Palmatolepis 

gracilis gracilis. 

The Daihua Formation (Upper part), 


limestone, bearing conodonts: Palmatolepis 

gracilis gracilis, P. g. signoidalis, P. g. expansa, 

Siphonodella praesulcata, Pseudopolygnathus 

trigonicus, Bispathodus stabilis, Protognathodus 

meischeneri, Palmatodella delicatula, Tripode- 

llus robustus, Spathognathodus supremus, 

Ozarkodina homoarcuata., Parawucklumeria sp. 

Sample Mh 12-Mh 13 (50 cm.) grey 

dense limestone, yielding conodonts: Palmat- 

olepis gracilis gracilis, P. g. sigmoidalis, P. g.


expansa, Spathognathodus werneri, Pseudopo- 

lygnatkus trigonicus, Palmatodella delicatula, 

Conchodontus ziegleri gen. et sp. nov., “Spath- 

ognathodus” dentilobus sp. nov., S. supremus, 

Pelekysgnathus sp., Parawucklumeria sp. 

2. The Bading section, Liuzhai commune, 

Nandan County, Guangxi. 

This section has not yet been measured in 

detail. The Wangyou Formation is composed of 

about two-meter-thick nodular argillaceous 

limestone bearing Siphonodella sulcata. The 

overlying strata of the Wangyou Formation 

consist of black thin-bedded marlstone. 

3. The Baping section, Nandan County, 

Guangxi. 

This section is situated at about 1 km. 

east of the Baping village of the Manchang 

commune, Nandan County, Guangxi. The 

Wangyou Formation is composed of small 

lenticular limestone with some mudstone. Its 

overlying rock is black crystalline limestone. 

The lithological characters of the Daihua 

Formation are the same as those in Muhua and 

Baping. 

4. The Lali section, Yishan County, 

Guangxi. 

The section is located at Xiaodong 

nearby Lali, Yishan County. The strata across the 

Devonian-Carboniferous boundary are mainly 

composed of nodular limestone and grey 

limestone. 

Discussion and Conclusion 

1. From above described four sections, 

it is obvious that the strata across the Devonian- 

Carboniferous boundary in southern Guizhou 

and northern Guangxi are very similar in litholo- 

gical characters, we use the same stratigraphical 

names for both areas, namely the Daihua 

Formation for the uppermost Devonian and the 

Wangyou Formation for the Lowermost 

Carboniferous. 

The Wangyou Formation is composed 

of nodular limestone. Its overlying black 

crystalline limestone at Baping and Muhua is 

only two-meter-thick. 

The Wangyou Formation is distributed 

widely in southern Guizhou and northern 

Guangxi. The lithological characters of the 

Wangyou Formation changed at places from 

nodular or small lenticular limestone to grey 

dense limestone (Muhua). The age of the 

Wangyou Formation is defined from Lower 

duplicata-Zone to sandbergi-Zone when it was 

established. From the data available now, the 

lower boundary should be the lower occurrence 

of S. sulcata, the upper boundary of the 

formation is diachron. The time interval of the 

Wangyou Formation is from sulcata-Zone to 

Lower crenulata-Zone. 

The lithological characters of the Daihua 

Formation in southern Guizhou and northern 

Guangxi are similar, We named the overlying 

black shale of the Daihua Formation as 

Changshun shale for the time being, Changshun 

shale is only a few centimeters thick, it is 

Devonian in age. 

2. Devonian-Carboniferous boundary 

The following three problems are worth 

notice when we discuss the Devonian- 

Carboniferous boundary of the Muhua section: 

a. The age of the Changshun shale. 

There are abundant specimens of 

Palmatolepis gracilis expansa in sample Mh 11, 

of which the upper limit is within the Middle 

costatus-Zone. Palmatolepis gracilis 

gonioclymeniae and Bispathodus ultimus which 

are characteristic for the Middle costatus-Zone 

have not been found in the Muhua section, but 

we have got Palmatolepis gracilis goniocly- 

meniae from near the top of the Daihua 

Formation at the Baping section (sample C18-2). 

It is uncertain whether the age of the Changshun 

shale is partly the Middle costatus-Zone or 

within the Upper costatus-Zone, but not 

extending to the topmost Devonian, although the 

“Changshun shale is definitely Devonian in age. 

b. The age of sample Mh 10-2. 

The first occurrence of S. sulcata is in 

sample Mh 10-1, sample Mh 10-2 contains 

typical Protognathodus-Fauna, which is consid- 

ered as representing a special biofacies, partly of 

the praesulcata-Zone without Proto. kuehni, 

partly of the sulcata-Zone with Proto. kuehni. 

One que-stionable specimen of Proto. kuehni 

(plate III, fig. 13) has been identified in sample 

Mh 10-2. If this specimen is truly Proto. kuehni, 

the Lowermost Carboniferous boundary should 

be below Mh 10-2, namely between the


Changshun shale and the Wangyou Formation., 

if there is no Proto. kuehni in sample Mh 10-2 

and there are S. praesulcata in Mh 10-2 and 

Proto. kuehni in Mh 10-1, then the 

Devonian-Carboniferous boundary would pass 

through homogeneous limestone, namely 

between Mh 10-1 and Mh 10-2, the Muhua 

section would be one of ideal potential stratotype 

for the Devonian-Carboniferous boundary. 

c. The relationship of the Changshun 

shale and the Wangyou Formation. 

It may be continuous deposits. But we 

could not exclude the possibility of a slight 

faunal hiatus between the Changshun shale and 

the Wangyou Formation with parts of Upper 

costatus-Zone and parts of Protognatkodus- 

Fauna missing. The reasons are as follows: 1. It 

is possible to find Proto. kuehni in sample Mh 

10-2, that means, a part of Protognathodus- 

Fauna, not containing Proto. kuehni, is missing. 

2. the age of the Changshun shale can't be 

precisely defined. 3. the bedding planes of the 

tops of the Daihua Formation and of the 

Changshun shale are waved, the thickness of the 

shale changed rapidly. 4. the layer Mh 10 is a 

limestone lens, its thickness changed, the 

horizon corresponding to sample Mh 10-2 

disappeared only two meters away from the most 

thickness of the lenses. 5. Changshun shale itself 

is an important symbol of the “globular event”. 

3. Conodont zonation in the Muhua 

section (see fig. 2 ) 

a. S. praesulcata occurs in sample Mh 

11 in the Daihua Formation. There are thousands 

of specimens of Palmatolepis gracilis gracilis, P. 

g. sigmoidalis, P. g. expansa, Pseudopolygnatkus 

trigonicus, etc. in every sample from Mh 24 to 

Mh 11, praesulcata-Zone corresponds to this 

interval. The first occurrence of praesulcata is 

within the Middle costatus-Zone in America. 

The base of the Middle costatus-Zone is defined 

by the lowest occurrence of B. ultimus and the 

top is defined by the highest occurrence of 

Palmatolepis gracilis gonioclymeniae (Ziegler, 

1962). Neither species has been recognized, 

however, at the Muhua section, there are 

abundant specimens of P. g. expansa, its highest 

occurrence is within the Middle costatus-Zone, 

therefore we can not rule out the possibility that 

this interval stratum belongs to the Middle 

costatus-Zone. The highest occurrence of S. 

praesulcata is within Lower duplicata-Zone 

(Mh8). 

b. Sample Mh 10-2 corresponds to 

Protognatkodus-Fauna, We couldn’t divide the 

fauna into upper and lower parts owing to the 

absence of reliable Proto. kuekni. The first 

occurrence of S. sulcata is in the sample Mh 

10-1, sample Mh 10-1 and Mh 10-2 belong to 

same limestone lenses with 9-30 cm. thick. 

c. The first occurrence of Lower 

dupticata-Zone is in sample Mh8. The boundary 

of Lower duplicata-Zone and Upper duplicata- 

Zone roughly lies between sample Mh6 and Mh5, 

because S. duplicata Morphotype 2 and S. 

obsoleta appeared in sample Mh5 and Mh 5-1, 

d. The sandbergi-Zone should begin 

from sample Mh 3, Dinodus fragosus and D. 

leptus have their lower occurrence in sandbergi- 

Zone(Mh3). 

e. There are only a few specimens of S. 

crenulata in sample Mh 2 but many specimens 

of S. sandbergi. We suppose the sample Mh2, per. 

haps. cut across sandbergi-Zone and Lower 

crenulata-Zone in collection (15 cm. thick.). 

4. The discovery of the conodont 

sequence from praesulcata-Zone to Lower 

crenulata- Zone provides a more refined basis 

for the subdivision of the Devonian- 

Carboniferous boundary and for the correlation 

of Lower Carboniferous stratigraphy in South 

China. The Devonian-Carboniferous boundary in 

pelagic facies of South China can be drawn 

between praesulcata- Zone and sulcata-Zone. 

Systematic paleontolgy 

Conchodontus Wang et Yin gen. nov. 

Type species: Conchodontus ziegleri gen. 

et sp. nov. 

12 specimens have been studied. All are 

well preserved and some ontogenetic stages can 

be observed. Species of Palmatolepis gracilis 

gracilis, P. g. sigmoidalis, P. g. expansa and 

Sipkonodella praesulcata have been found in 

association with new species here described. 

Rounded to elongated (anteriorly to 

posteriorly) platform with one low middle carina 

and large irregular nodes on oral surface. 

Anterior end rounded or with distinct projection


as a“biak” or entire specimen elongated. 

Specimen strongly arched to form convex oral 

surface. Middle carina low from anterior to 

posterior margin, composed of irregular nodes. 

Nodes either randomly arranged or in definite 

pattern. Posterior margin wide and smooth. 

Aboral surface concave with prominent deeper 

pit into anterior extension. Growth lines dn 

aboral surface can be seen. 

Conchodontus ziegleri gen. et sp. nov. 

Subrounded to elongated platform with 

anterior projection and irregular nodose surface. 

Platform subsymmetrical or unsymmetrical. Low 

middle carina from anterior end to posterior 

composed of somewhat fused nodes. Nodes 

randomly arranged on anterior platform but 

somewhat radiately arranged on posterior. 

Posterior margin wide, smooth, and thin in 

thickness. Platform thickness increases rapidly 

from posterior to anterior extension. One small 

specimen studied here is subrounded; a middle 

carina and two wide depressions at both sides of 

carina, two large specimens have only one 

depression on left side of posterior carina. 

Anterior extension like brachiopod 

“biak”, its aboral surface like “interarea” which 

is smooth. Aboral surface strongly arched and 

growth lines concentrical. A pit at anterior end 

into“biak” and closed by “interarea”. Margin of 

aboral surface at anterior angular, posterior 

margin thin. 

Locality and horizon: Muhua, 

Changshun County, Guizhou Province, Upper- 

most Devonian, The Daihua Formation, 

Conodont zonation: praesulcata-Zone or 

Middle-Upper costatus-Zone. 

Conchodontus sp. nov. 

One specimen only. Middle carina more 

distinct. Aboral surface anterior margin circular. 

Right posterior margin broken. Other characters 

similar to those of Conchodontus zicgleri gen. et 

sp. yon. 

Locality and horizon: Baping, Nandan 

County, Guangxi. Daihua Formation. Conodont 

zonation: praesulcata-Zone. 

“Spathognathodus” dentilobus sp. nov. 

“Spathognathodus” dentilobus sp. nov. is 

characterized by extremely large straight outer 

lobe with a very thin middle ridge and one to 

three denticles on it, and an indistinct or very 

small inner lobe. Basal cavity is Strongly 

asymmetrical, near the posterior of blade, and 

confined to the area under the lobes. Anterior 

blade straight and five times longer than the 

post-blade. Single denticle row is uneven with 

the highest and largest denticles at the anterior. 

From the basal cavity to the posterior end the 

denticles gradually decrease in height. 

The position of the basal cavity of new 

species is near the posterior, as opposed to 

characteristic of Ozarkodina asymmetricus 

(Bischoff and Sanneman). It differs from the P 

element of Amydrotaxis johnsoni by the 

existence of the denticles on the outer lobe, and 

it is distinguished from Ozarkodina transitains 

by relative small inner lobe and the position of 

the basal cavity. 

Locality and horizon: Muhua, 

Changshun County, Guizhou. The Uppermost 

Devonian, the Daihua Formation. Conodont 

zonation: praesulcata-Zone or Middle-Upper 

costatus-Zone.


图版说明 

标本存放在中国科学院南京地质古生物研究所,登记号 80798—80881 

图版 I 

1—2,9.Siphonodella praesulcata Sandberg,1972 

Mh8/80798,×26,Mh6/80799,×52; Mh8/80806, 

×52.睦化;王佑组 

3.Siphonodella cooperi Hass,1959,Morphotype 1 

ADM20/80800,×26.巴平;王佑组。 

4,19—20.Siphonodella sandbergi Klapper,1966 

Mh2/80801,×26;Mh2/80816,×26;Mh2/80817, 

×26.睦化;王佑组。 

5,17.Siphonodella obsoleta Hass,1959 

ADM20/80802,×26;ADM5/80814,×26.巴平; 

王佑组 

6.Siphonodella isosticha-obsoleta 

C36-1/80803,×26.巴平;王佑组 

7.Siphonodella isosticha (Cooper) 1939 

ADM19/80804,×26.巴平;王佑组。 

8.Siphonodella sulcata (Huddle)1934 

Mh8/80805,×52.睦化;王佑组。 

10.Siphonodella duplicata (Branson et Mehl)1934,Mo- 

rphotype 1 

Mh8/80807,×52.睦化;王佑组。 

11,15.Siphonodella duplicata (Branson et Mehl) 1934, 

Morphotype 2 

LX5-1/80808,×52;Mh4/80812,X.拉利,睦化; 

王佑组。 

12.Siphonodella lobata (Branson et Mehl) 1934 

Mh2/80809,×26.睦化;王佑组。 

13—14.Siphonodella cooperi Hass,1959,Morphotype 

2 

Mh2/80810,×26;ADM20/80811,×26.睦化, 

巴平;王佑组。 

16.Siphonodella duplicata sensu Hass,1959 

Mh8/80813,×26.睦化;王佑组。 

18,21.Siphonodella quadruplicata (Branson et Mehl) 

1934 

ADM21/80815,×26;Mh6/80818,×26.巴平, 

睦化;王佑组。 

22.Siphonodella crenulata (Cooper) 1939,Morphotype 

2 

C36-1/80819,×26.巴平;王佑组。 

23—24 . Siphonodella crenulata (Cooper) 1939 , 

Morphotype 1 

ADM20/80820,×26;ADM19/80821,×26.巴平; 

王佑组。 

图版 II 

1.Polygnathus communis carinus Hass,1959 

Mh10-2/80822,×26.睦化;王佑组。 

2.Polygnathus communis communis Branson et Mehl, 

1934 

Mh10-2/80823,×26.睦化;王佑组。 

3.Polygnatnus purus purus Voges,1959 

LX5-1/80824,×26.拉利;王佑组。 

4—5.Polygnathus purus stublanus Voges,1959 

LX5-1/80825,126:Mh8/80826,×126.拉利, 

睦化;王佑组。 

6.Polygnathus delicatula Ulrich et Bassler,1926 

ADM20/80827,×26.巴平;王佑组。 

7.Polygnathus lobatus Branson et Mehl,1934 

LX5-1/80828,×26.拉利;王佑组。 

8.Polygnathus longiposticus Branson et Mehl,1934 

ADM20/80829,×26.巴平;王佑组。 

9.Pseudopolygnathus triangula triangula Voges,1959 

Mhg-1/80830,×26.睦化;王佑组。 

10.Polygnathus inornatus Branson,1934 

ADM5/80831,×26.巴平;王佑组。 

11—13.“Spathognathodus” dentilobus sp.nov. 

Mh19/80832,×26(Paratype); Mh19/80833,×26 

(Paratype);Mh13/80834,×26 (Holotype).睦化; 

代化组。 

14—15. Pseudopolygnathur multiariatus Mehl et 

Thomas,1947 

Mh5/80835,×26;Mh5/80836,×26.睦化;王佑 

组。 

16.Pseudopolygnathus sp. 

Mh8/80837,×26.睦化;王佑组。 

17.Pseudopolygnathus triangula pinnata Voges,1959 

Mh4/80838,×26.睦化;王佑组。 

18,23.Pseudopolygnathus dentilineatus Branson, 1934 

Mh8/80839,x26;Mh8180844,×26.睦化;王 

佑组。 

19—24.Pseudopolygnathus vogesi Rhodes,Austin et 

Druce,1968 

Mh8/80840,126;Mh3/80845,×26.睦化;王佑 

组。 

20—22.Pseudopolygnathus primus Braonson et Mehl, 

1934 

Mh4/80841,×26;LX9/80842;Mh2/80843,×26.睦 

化,拉利;王佑组。 

25.Pseudopolygnathus cf.dentilineatus Branson,1934 

LX7-2/80846,×52.拉利;王佑组。 

26.Pseudopolygnathus cf.breuipennatus Ziegler,1962 

LX9/80847,×52.拉利;王佑组。 

27.Dinodus leptus Cooper,1939 

Mh2/80848,×26.睦化;王佑组。 

28.Blictognathus bialata Branson et Mehl) 1934


C36—1/80849,×26.巴平;王佑组。 

29.Dinodus fragosus (E. R.Branson)1934 

Mh2/80850,×26.睦化;王佑组。 

图版 III 

1—2.Palmatolepis gracilis gracilis Branson et Mehl, 

1934 

Mh11/80851,×26;Mh11/80852,×26.睦化;代 

化组。 

3—4.Palmatolepis gracilis sigmoidalis Ziegler,1962 

Mh11/80853,×26;Mh11/80854,×26.睦化;代 

化组。 

5.Palmatolepis gracilis gonioclymeniae Müller,1956 

C18—3/80855,×26.巴平;代化组。 

6—8 . Palmatolepis gracilis expansa Sandberg et 

Ziegler,1979 

Mh11/80856,×26;Mh11/80857,×26;Mh11/80858, 

×26.睦化;代化组。 

9. Pelekysgnathus guizhouensis Wang et Wang,1978 

Mh11/80859,×26.睦化;代化组。 

10—11.Bispathodus costatus (E.R.Branson) 1934, 

Morphotype 2 

6511-1c/80860,×26;6511-2c/80861,×26.巴定; 

代化组。 

12,14—15.Protognathodus kockeli (Bischoff)1957 

Mh10-2/80862,×26,Mh10-2/80864,×26;Mh10— 

2/80865,×26.睦化;王佑组。 

13.Protognathodus kuehni (?) Ziegler et Leuteritz,1970 

Mh10-2/80863,×26.睦化;王佑组。 

16.Protognathodus collinsoni Ziegler,1969 

Mh10-2/80866,×26.睦化;王佑组。 

17.Protognathodus meischneri Ziegler,1969 

Mh10-2/80867,×26.睦化;王佑组。 

18.Spathognathodus inornatus (Branson et Mehl) 1934 

Mh11/80868,×26.睦化;代化组。 

19.Spathognathodus supremus Ziegler,1962 

Mh11/80869,×26.睦化;代化组。 

20.Polygnathus communis stylensis Lipnjagov,1979 

LX10-2/80870,×26.拉利;王佑组。 

21.Polygnathus vogesi Ziegler,1962 

LX10-2/80871,×26.拉利;王佑组。 

22.Bispathodus aculeatus aculeatus (Branson ct Mehl) 

1934 

Mh10-1/80872,×26.睦化,王佑组。 

23.Pinacognathus profunda Branson et Mehl,1934 

Mh9/80873,×26.睦化,王佑组。 

24.Spathognathodus planiconvexus Wang ct Ziegler, 

1982 

Mh8/80874,×26.睦化,王佑组。 

25.Pseudopolygnathus trigonicus Ziegler,1962 

Mh11/80875,×26.睦化,代化组。 

26—30.Conchodontus ziegleri Wang et Yin gen. et sp. 

nov. 

Mh13/80876,×52,(Paratype);Mh11/80877,×52, 

(Paratype);Mh11/80878,×52,(Holotype);Mh13: 

80879,×52,(Paratype);C18-1/80880,×52,(Pa- 

ratype),睦化、巴平;代化组。 

31.Conchodontus sp.nov. 

C19-1/80881,×98.巴平,代化组。

华南浮游相区早石炭世早期牙形刺分带和泥盆系、石炭系的分界

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