276 The American Geologist. May, 100% 
much stained with iron oxide as are the narrow talc belts in 
the serpentine areas of the north. , 
There are also quite a number of narrow strips of coarsely 
crystalline actinolite, precisely as in the Abrams mica schist. 
These are not the result of contact metamorphism as in the™ 
Franciscan series, but of regional thermo-metamorphism act- 
ing on strata of the proper chemical composition to yield them. 
The major portion of the series is a true mica schist like 
the bulk of the Abrams mica schist, but along the crest of the 
mountain where occur the calcareous, chloritic and actinolitic 
members interbedded with the regular mica schists (an asso- 
ciation characteristic of the transition from the Abrams mica 
schist to the Salmon hornblende schist) there are layers of a 
dull greenish, coarsely granular rock which resembles the low- 
er stratum of the Salmon hornblende schist. It apparently 
consists of somewhat rounded grains of quartz separated and 
surrounded by thin folia of blade-shaped crystats of dark 
green and black hornblende. Some mica is present in this 
Sierra Pelona representative; otherwise it* is identical with 
the Salmon schist above mentioned. Nothing of the kind was 
seen in the Sierra Nevadas. 
At the summit of the Sierra Pelona occurs a vein, partly 
of fine granular, transparent quartz and partly of irregular 
masses of iron oxide of a black color with cavities lined with 
vellow ochre, a kind of vein peculiar to the Abrams mica schist 
in the Klamath region, increasing the probability of the Pelona 
and Abrams schists being identical. 
Che estitzeted thickness of the dark colored schists is 
3,000 feet, making 5,000 feet forthe series—the Pelona Schist 
Series. 
About the head of the Texas cafion, the schists of the 
Sierra Pelona stand nearly vertical, but locally leaning over 
to one or the other side, the general strike being east-west. 
The dark-colored schists form the summit and the light yellow 
schists, the southern flank. Near the base of the mountain 
come in apparently schists and quartzytes which are much 
stained with iron, give the surface a buff color, and in places 
they seem to be much less metamorphic than the schists in the 
bulk of the mountain. Some spots appear decidedly like blue 
cherts of the Lower Slate series in the Kiamath region, only 
