Kvamshestens devonfelt. 87 



dorite rock (anorthosite), pyroxenite, garnet bearing amphibolite, 

 epidote rock, marble, phyllite (partly coalbearing), greenschists, 

 quartzites and quartzschists. The rocks in the pebbles are essenti- 

 ally the same which we know from the present surrounding rocks 

 of the area. 



Some of the smaller pebbles are only mineral fragments. In 

 these the following minerals are represented: microperthite, mi- 

 crocline, orthoclase, plagioclase, quartz, hornblende, epidote, mag- 

 netite, zircon and calcite. All these minerals we find in the 

 abovementioned rocks from wich it is most likely that they originate. 



The consistence of the different pebbles as well as their form 

 suggest that the material has been transported only a short di- 

 stance. In some places one gets the impression that it has been 

 formed "in situ" by destruction of the substratum, in other places 

 the material most likely has been brought down into the basin 

 by powerfull but intermittent torrents. 



The boundary between the basal conglomerates and the 

 underlying rock is a thrustplane which can be seen at fig. 4 and 5, 

 from the south side of Kvamshesten. Fig 3 shows a detail section 

 from the same mountain, where the underlying crystalline schist 

 has been pressed into the Devonian conglomerate. The crushing 

 of the lower part of the basal conglomerate may be seen at the 

 microphoto fig. 2. 



In the uppermost part of the basement conglomerates there 

 are layers of sandstone alternating with layers of conglomerate 

 so that we get a transition to 



The series of red and green sandstones. 



(Page 32-49). 



This important series of strata extends from the north side 

 of the "Kvamshesten" and westwards to Tjønnebotn (T. on the 

 map) south of Eidsfjeld. From here the series can be followed 

 on the west and north side of the Eidsfjeld and on the south 

 side of the lake Bjørnevand. 



The series consist of alternating red and grey-green sand- 

 stones, the latter partly containing conglomerates with rolled peb- 

 bles (fig. 15 and 21). The green sandstones have got their colour 

 especially from chlorite and epidote which are predominant in the 

 cement. The red sandstones also contain much chlorite and epi- 



