48 



I'KNTTl KSKOI.A. 



M.-N. Kl. 



( )n AasniH-s near Bryggen it is a.ssc)ciated with a finely banded eclogite 

 and at another point it forms an 8 meters thick lens in which the garnet 

 is somewhat concentrated in certain bnnds. 'j'he garnets, in both the last- 

 named occurrences, are rounded .md <>! larger size than they are in the 

 common |)yroxene-eclogite. When emlx ddid Id tin large crystals of amphi- 

 Ixijc, they ai-c surrounded by thin zones of deeper green hornblende forming 

 the continuation of the colourless amphibole. Zoisite is present as large prisms. 



The eclogites of Duen type in Vanelvsdalen commonly contain irregular 

 patches or nodules of such amphibole-eclogite. 



^ Fcloi 



ite-pegmatite. 



Amphibolilized 

 eclogite-pegmatite. 



Eclogite. 



Amphibolitizcd bound- 

 ars'-zones and cracks. 



Gneiss. 



Fig. 4. Eclogite-pegmatite in gneiss. (Irytingvaag, Selje. 



Many eclogites contain similar pale-green amphibole (smaragdite) as 

 large crystals besides dominant pyroxenes, and may be understood to be 

 transitional between the true pyroxene-eclogites and the amphibole-eclogites. 

 In such rocks there is nowhere an}' proof of posterior alteration of the 

 pyroxenes into amphibole. It seems more probable that the amphibole has 

 originated at the later stage of the magmatic crystallization. 



In the Gangeskar eclogite the pyroxene and garnet both present 

 themselves as relics, and the development of the rock probably was some- 

 Ayhat as follows: Garnet and ortho- and clinopyroxene had crystallized out 

 from the magma in the usual way, but the consolidation, did not end with 

 these phases, probably because mineralizers were present in larger amounts 

 than usually and residual magma was still present, when the temperature 

 had sunk btlow the stability limit of the eclogite faciès. The clinoaniphi- 



