224 BULLETIN: MUSEUM OF COMPARATIVE ZOOLOGY. 
in eastern Scania, present in western Scania, well developed in Viaster- 
gétland at Hunneberg and Kinnekulle, and present though less 
developed in other places. As previously noted, the shale is absent 
at Ekedalen, and Fearnsides has pointed out that the shale thickens 
in going away from Skéofde and Ekedalen. Munthe gives the follow- 
ing thicknesses at places on the Skofde sheet of the Geologic Map: 
Ulunds, .6 meters, Baickagarden .23 meters, Kapplunda .2 meters, 
Persberg, absent, Skultorps Norra .9 meters. At Klefda in the west- 
ern Falbygden region, not far from Falk6ping, the thickness is three 
meters, at Hunneberg, eleven meters (capped with diabase), and at 
Kinnekulle, ten meters. As to fauna, it is only in eastern Scania that 
the four subfaunules are developed. Here one sees, in descending 
order:— (4), zone of Isograptus gibberulus, (3), zone of Phyllograptus 
angustifolius. (2), zone of Didymograptus balticus. (1), zone of 
Tetragraptus phyllograptoides. 
In connection with the thinning of the shales toward Ekedalen it is 
important to note that at Hunneberg one finds the zones 1 and 2, at 
Kinnekulle 1, 2, and 3, the Limbata limestone succeeding the shale, 
but in the thin sections in the Sk6fde area Phyllograptus angustifolius 
is reported as the most common graptolite, indicating the presence 
there of zone 3. In other words, the shale has thinned by the loss of 
the lower members, thus showing overlap in that direction and sus- 
taining the idea that there was an island of Cambrian strata here in 
early Ordovician times. The Ceratopyge formation also thins in this 
direction, as shown by Munthe’s measurements in the Skéfde sheet: 
Ulunda .3 meters, Backagarden .12, Kapplunda .4, Persberg .3, 
Skultorps Norra .9 and Skultorps Sodra .15. It has been argued 
(Wiman, 90) that the foot of conglomeratic and glauconitic limestone 
resting on the Cambrian at Ekedalen represented the Ceratopyge 
limestone, but this seems very improbable both on faunal and strati- 
graphic grounds. 
It has been suggested that the lower part of the Lower Didymo- 
graptus beds replace the Ceratopyge limestone in certain regions, but 
the very general occurrence of the Tetragraptus phyllograptoides 
faunule in shales resting on the youngest of the Ceratopyge zones 
negatives this idea. That the Limbata limestone does replace the 
upper part of the shale is, however, readily shown by the occurrence of 
the fauna of the Isograptus gibberulus subzone in or above the Limbata 
limestone on Oeland. 
In connection with the development of the Orthoceras limestone, 
certain things should be noted. For instance, in those sections where 
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