1914 — 15] Fj eldby giringen mellérn Sørfjorden og Samnangerf jorden. 233 



tains numerous larger or smaller folia of mica (mainly muscovite, 

 serieite, more seldom biotite) and some quartz, which is segregated 

 either as lenses and streaks, or occurs in the phyllite itself together 

 with mica, felspar, and a number of other minerals. Some phyllites 

 are garnet-bearing. At Hisdal. Aadland, Nordvik and Fitjevand 

 the phyllite is more or less carbonaceous. This kind of alum-phyl- 

 lites does not seem to belong to espeeial niveaus, which can be 

 followed contiauously through the whole area, but has attained to 

 its present place between the other phyllites by inversion. The 

 whole series of layers of phyllites show a "Schuppen-structur", the 

 details of which cannot be studied without difficulty owing to the 

 folding which has repeatedly tåken place, and on account of the 

 dipping of the folding-axis, and finally because of the subsequent 

 erosion, which at various places may attain various depths. In some 

 localities we see a distinct interchange of the ordinary phyllite and 

 various schistose, hornblende-bearing rocks rich in felspar and often 

 containing garnet. The section in flg. 46 which has been tåken 

 at Skuteviken near Kvennes, south of Aadland, exhibits such an 

 interchange of layers. 



By regarding the rocks of this section we get the impression 

 that the phyllite has been penetrated by granite-magma, and partly 

 by dissolved quantities of albite. Some parts of one of the zones 

 rich in felspar are easily split up along joints where mica and dark 

 hornblende-needles are the essential components. Between the joints 

 is seen a fine-grained, whitish or greyish rock with greenish-black 

 hornblende-needles and some garnets. The rock reminds one a good 

 deal of a type of granitic dyke-rocks in the Samnanger-area. Its 

 structure may be seen in flg. 49. 



Extending from the tract south-west of Skar and northwards 

 to Histadsfjeld there is a zone of some various rocks which I have 

 designated as chloritic schists, and which partly are bordered 

 by faults. 



At the farms Landsvik, Haga and Stensland there extends a 

 zone of rocks which through invertion is brought in between the 

 phyllites. As may be evident from the section, fig. 51, we have 

 here an alternation of various rocks, of which the chloritic schists 

 with partly conglomerate-structure and the schistose saussurite- 

 diabases constitute the principal mass. I look upon these rocks 

 as strongly metamorphosed basic tuffs with volcanic conglomerates 

 and old volcanic currents. In the schistose saussurite-diabases are 



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