54 BRITISH AVONIAN CONODONT FAUNAS 
the genus is present in Devonian faunas in southwestern England. We stress that 
these are negative data, however ; indeed, it seems possible that a few Lower 
Carboniferous faunules may contain indigenous palmatolepids. 
It is possible that our Lower K faunas are close to the fauna briefly described by 
Bouckaert & Ziegler (1965, Chart 9, p. 25) from the section at Huy 2 in Belgium. 
The highest part of this section (19) contains a new genus (not described, illustrated, 
or mentioned in the text) together with S. aculeatus E. R. Branson and Pseudopoly- 
gnathus dentilineatus E. R. Branson. The first of these two species may represent 
S. plumulus. Bouckaert & Ziegler also record from the same sample (1965 : 17), a 
single specimen of a form “ which seems to represent a new trend evolved from 
Spathognathodus costatus’’’ (Pl. 4, fig. 12 and p. 27 : Pseudopolygnathus sp.). This is 
close to our Pseudopolygnathus vogesi sp. nov. A Lower Tournaisian age for this 
part of the Belgian section has been suggested by Conil (1964) on the basis of the 
foraminifera, and Streel (1966) states that the spores indicate a Devonian age. 
Klapper & Sandberg (1967 : B 52) have found the genus Patrognathus in a very 
thin interval of strata in Wyoming (the Windy Gap Formation). It is associated 
with Siphonodella sulcata, a species that was also recovered by these authors from 
the upper part of the G. kockeli-P. dentilineatus conodont zone in Germany (Voges 
1959, text-fig. 1, Samples 3 and 4). 
An undescribed conodont fauna from the Lower Pilton Beds contains Spatho- 
gnathodus plumulus sp. nov., Pseudopolygnathus vogesi sp. nov. and representatives of 
the genus Clydagnathus (J. W. Williams, personal communication). The Lower Pilton 
Beds are considered to be of Wocklumeria age (Goldring 1955). However, no speci- 
mens of the genus Patrognathus have as yet been found in the Lower Pilton Beds. 
Thus the Lower Limestone Shale appears to be younger than the Lower Pilton Beds. 
The conodont fauna of the Lower Pilton Beds is unlike the fauna from the Wock- 
lumeria to VI Zone described by Ziegler (1962). It is closer to the fauna described 
by Bouckaert & Ziegler (1965), from the uppermost Fammenian at Huy. 
All the evidence points to the conclusion that a gap in the conodont sequence is 
present in the type section of the Devonian—Carboniferous boundary in the Hénnetal 
railway cutting. The Huy section of Fammenian age is younger than the type to VI 
strata at Hénnetal, but on goniatite and spore evidence it is still Devonian. The 
base of the Lower Limestone Shale is younger than the Huy section (on the basis of 
the absence of the genus Patyvognathus in the Huy section), but is older than the base 
of the Tournaisian in the Honnetal railway cutting. 
Thirty feet above the base of the K section in the North Crop a single specimen of 
Elictognathus has been found. £Elictognathus makes its first appearance in North 
America at the base of the Siphonodella sulcata Assemblage Zone which is near the 
the base of the Hannibal Formation, and is correlated with the middle part of the 
Lower Carboniferous Cu I Zone of Western Europe (Collinson, Scott & Rexroad 
1962). 
Associated with Elictognathus in the Pseudopolygnathus vogesi—Clydagnathus 
Assemblage Subzone of the Avonian is Pseudopolygnathus vogesi sp. nov. This 
species is characteristic of the lower part of the Lower Carboniferous Cu I Zone of 
