88 E. 0. Teale: 



It may be of some significance, therefore, that we find in this; 

 line other complex Lower Palaeozoic inliers, whose structural de- 

 tails and relatioiiships a.re still a subject of controversy, and pro- 

 vide promising scope for further work. 



The pho«phatic deposits at Flannery's, near Mansfield, and the- 

 associated sedimentary rocks form one of the most interesting inliers 

 in question. 



Some very fragmentary fossils were obtained some years ago 

 from the phosphatic material, consisting chiefly of Salterella, and 

 obscure trilobite remains. The fossils were very unsatisfactory, but 

 were regarded by Professor Gregory as probably Cambrian. Pro> 

 fessor Skeats and Dr. Summers have obtained both Upper and 

 Lower Ordovician, and Mr. A. M. Howitt Lower Ordovician grapto- 

 lites in such close proximity to the spot from which the trilobite 

 remains were found that the geology is clearly complex, and the re- 

 sults of more detailed work should be of considerable interest. 



Another area requiring further attention is in the Upper Howqua 

 Valley, al; i-uch a position that the extension of the Cambrian axis 

 of the Wellington region might be expected to appear. 



Mr. A. M. Howitt (22) made a flying visit to this region about 

 eleven years ago, and recorded the occurrence of cherts, which were 

 regarded as^ Cambrian, phosphate rock, amphibolites and serpen- 

 tine of undetermined age, also Silurian slates and sandstones. 



The relationship of these rocks has recently been discussed by the 

 author in the Proc. Roy. Soc, Vic. 



Silurian. — The rocks of this series consist chiefly of alternating 

 quartzitic sandstones and greenish sandy shales. Some of the latter 

 have a marked rubbly to splintery mode of weathering, and by 

 oxidation are frequently rusty broAvn near the surface. Ihey dip 

 at high angles, and have been folded along numerous axiall lines in 

 a general N.N.W., to N.W. direction. Though they have been sub- 

 jected to much folding and even overfolding, as shown in the 

 Dolodrook, below Thiele's Creek junction (Photo. 2), the intense 

 contortion which is such a marked feature of the Ordovician is as 

 a rule absent. 



The actual contact between the Ordovician black slates can be 

 seen at several outcrops. Three of theae are worthy of mention. 

 One is in Blytli's Gully (Loc. D.), about 20 chains N.N.W. from the 

 Wellington-Dolodrook Junction. Another is in the bed of a steep 

 tributary gully of the Wellington, about a mile N.W. of the above- 

 named junction (Loc. E.), and the third is in Thiele^s Creek, about 



