524 GEOLOGY AND PETROGRAPHY OP CLARENCETOWX-PATERSON DISTRICT, ii., 



W. and an overlap occurs in the beds. A careful examination up the coui-se of 

 Dunn's Creek failed to show any signs of faulting, although the line of the creek 

 and also the junction of the toscanite and overlying tillites are in the direction 

 of the fault, wherefore it seems likely that the fault is connected with the steep 

 flexure existing along the stream. Of further interest are the occurrences of 

 Paterson toscanite lying fairly flatly a little to the north, and the outlier of 

 Lower Marine Beds to the east. These Penno-Carboniferous rocks must exist 

 in a basin-shaped dejjression as they disappear in the direction of plunging of 

 the syncline although the grade of the surface is not steep. 



Mention of the structure of Hungi-y Hill can now be made. Here there is a 

 strike fault indicated by the occurrence of the lower portion of the Glacial Stage 

 surrounded by the Paterson toscanite. The fault has a throw of 250 feet to the 

 north, and the stratigTaphical displacement at the point Y is 300 feet. The fault 

 is lost in the alluvium of the Paterson River to the west and its effects to the east 

 are uncertain. One hesitates to join this fault to the one just previously 

 described on account of the undisturbed strata between the ends of the fault as 

 shown on the map. F2 possesses a small branch about midway along its extent, 

 the hypersthene-pitchstone outcrops serving to indicate this. 



Fault Fa F3. — This long fault is encountered on the Seaham-Paterson road 

 where it strikes north. It can then be traced, with a fair amount of ease, from 

 Butterwick to the north, the strike becoming N.N.E. The consideration of the 

 positions of the Paterson toscanite and of the Volcanic Stage lavas near Glenoak 

 gives adequate evidence of its position and extent. Some very locally disturbed 

 areas are to be found, high and discordant dips being obtained. The throw in 

 the north is about 650 feet while in the south it is of the order of 900 feet, the 

 west being the downthrow side. 



A small branch fault from Fs occurs near Oakendale, an actual scarp being 

 discernible; the signiflcance of this will he considered under the physiography 

 section. 



Fault F4 F4. — Near Glenoak one has not to travel more than half a mile east 

 from F3 before another large fault is encountered. This has a trend essentially 

 parallel to F3, the downthrow side being, as in the ease of Fi and F2, to the 

 east. The total horizontal displacement ("shift" of some writers) is well shown 

 by considering the two toscanite units, in the Glacial and Volcanic Stages re- 

 spectively. The fault appears to be of the type in which there is a sag, the 

 throw decreasing on either side of the sag-point. In this case the maximum 

 throw is approximately 1,200 feet. 



Fault F-i. — This fault may be traced from the Limeburner's Road on the 

 north, through the country east of the Gilmore Ridge, to the flat swampy laid 

 known as Balaeara Swamps, the downthrow side being to the west. As a result 

 of this fault the strata to the east of the Williams River have been duplicated 

 and the Burindi Series has been brought to light by erosion. Beds of the Glacial 

 Stage appear against the Burindi Series and at the point where the line P Q R S 

 crosses the fault there is a stratigTaphical displacement of 4,500 feet. The general 

 throw of the fault is 6,200 feet, and the existence- of this heavy fault explains 

 the very great apparent thickness determined by Jaquet for the easterly dipping 

 beds along this section (Jaquet, 1901). 



There is no doubt that the fault in question is continued a long way to the 

 south and, after passing the region of the Balaeara Swamps, it trends down the 

 present course of the Lower Williams River. It is, therefore, the same fault 

 mentioned by Professor David in 1904, who, writing of the Carboniferous strata 



