THE   CORDILLERAS.  783 
Peale,46  in  1873,  states  that  the  base  of  the  mountains  near  Ogden 
is  for  the  most  part  a  red  syenite,  which  passes  into  granite  and 
gneiss,  and  contains  in  places  veins  of  hornblende,  quartz,  and  spec- 
ular iron.  The  granites  of  Cottonwood  Creek  are  conspicuously 
bedded,  the  dip  being  about  50°  or  70°  to  the  east,  and  they  contain 
rounded,  pebble-like  masses  of  a  dark  color  inclosed  within  the  gray 
matrix.  These  granites  are  cut  by  veins  of  feldspar.  The  pebble- 
like masses  suggest  that  the  formation  is  metamorphic. 
Bradley,47  in  1873,  regards  the  core  of  the  Wasatch  as  metamor- 
phic. The  occurrence  of  angular  and  rounded  patches  of  dark  mate- 
rial in  the  granite  of  Little  Cottonwood  Canyon  is  taken  as  evidence 
that  these  were  pebbles  of  a  conglomerate  before  its  metamorphism. 
The  rocks  are  chiefly  hornblende  gneiss  and  syenite,  with  quartz 
veins. 
Howell,48  in  1875,  states  that  in  Rock  Canyon,  near  Provo,  pebbly 
chlorite  schist  is  unconformably  below  hard  quartzite. 
Emmons  (S.  F.),35  in  1877,  describes  the  Wasatch  Range  as  a 
sharp  north-south  anticlinal  fold  over  preexisting  ridges  of  granite 
and  unconformable  Archean  beds,  the  axis  being  bent  and  con- 
torted by  longitudinal  compression  so  that  at  times  it  assumes  a 
direction  approximately  east  and  west.  In  connection  with  the  fold- 
ing is  a  widespread  system  of  faulting  and  dislocation,  in  a  direction 
generally  parallel  to  the  main  line  of  elevation,  which  has  cut  oil  and 
throAvn  down  the  western  members  of  the  longitudinal  folds  and  the 
western  ends  of  the  transverse  folds,  and  they  are  now7  buried  beneath 
the  valley  plains.  In  the  northern  region  is  a  second  broad  anti- 
clinal fold  to  the  east  of  the  main  line  of  elevation.  This  mountain 
range  occupies  the  line  of  former  Archean  uplift,  around  which  were 
deposited  30,000  or  40,000  feet  of  practically  conformable  beds  ex- 
tending upward  from  the  Cambrian  to  the  Jurassic.  At  the  base  of 
the  Paleozoic  is  the  Cambrian  formation,  which  has  a  small  thick- 
ness of  calcareous  slates  bearing  Primordial  fossils  and  a  great  thick- 
ness of  white  quartzite,  including  a  few  micaceous  beds  and  argillites, 
the  whole  being  12,000  feet  thick.  The  granite  mass  constituting 
the  center  of  the  Wasatch  was  not  protruded  through  the  sedimen- 
tary rocks,  but  the  latter  were  deposited  around  them,  and  their 
present  conditions  are  due  to  subsequent  elevation,  flexure,  disloca- 
tion, and  erosion. 
In  the  Cottonwood  canyons  is  a  large  mass  of  granite  which  shows 
a  conoidal  structure,  and,  while  massive,  has  distinct  plane-  of  cleav- 
age which  dip  50°  W.  It  is  a  white,  rather  coarse-grained  granite, 
dotted  here  and  there  with  round  black  spots  where  there  ha-  been  a 
concentration  of  the  dark-green  hornblende,  which  i-  a  prominent 
constituent  of  the  mass.     On  the  western  flanks  of  the  Cottonwood 
