﻿4-8 
  NEW 
  YORK 
  STATE 
  MUSEUM 
  

  

  the 
  whole 
  State 
  was 
  then 
  upraised 
  practically 
  without 
  folding, 
  and 
  

   the 
  conditions 
  were 
  certainly 
  favorable 
  for 
  extensive 
  fracturing 
  of 
  

   the 
  strata. 
  

  

  Any 
  fault 
  scarps 
  or 
  ridges 
  produced 
  during 
  or 
  at 
  the 
  close 
  of 
  

   the 
  Paleozoic 
  must 
  have 
  been 
  quite 
  or 
  nearly 
  obliterated 
  during 
  the 
  

   long 
  Mesozoic 
  period 
  of 
  erosion. 
  If 
  so, 
  how 
  do 
  we 
  account 
  for 
  the 
  

   present 
  Adirondack 
  ridges 
  which 
  follow 
  fault 
  lines 
  ? 
  As 
  a 
  result 
  of 
  

   the 
  uplift 
  of 
  the 
  Cretacic 
  peneplain 
  one 
  or 
  both 
  of 
  the 
  following 
  

   things 
  happened, 
  namely, 
  either 
  that 
  there 
  was 
  renewed 
  faulting 
  

   or 
  that, 
  as 
  a 
  result 
  of 
  unequal 
  erosion 
  (due 
  to 
  differences 
  in 
  rock 
  

   character) 
  on 
  opposite 
  sides 
  of 
  the 
  faults, 
  the 
  old 
  fault 
  scarps 
  were 
  

   renewed. 
  It 
  is 
  quite 
  certain 
  that 
  both 
  things 
  occurred 
  and 
  thus 
  

   we 
  account 
  for 
  the 
  present 
  Adirondack 
  fault 
  ridges. 
  That 
  some 
  

   of 
  the 
  faulting 
  actually 
  dates 
  from 
  the 
  uplift 
  of 
  the 
  Cretacic 
  pene- 
  

   plain, 
  or 
  possibly 
  even 
  later, 
  is 
  proved 
  by 
  the 
  existence 
  of 
  certain 
  

   fault 
  cliffs 
  in 
  perfectly 
  homogeneous 
  rock 
  masses, 
  and 
  by 
  the 
  fact 
  

   that 
  many 
  of 
  the 
  tilted 
  fault 
  blocks 
  have 
  been 
  little 
  modified 
  by 
  

   erosion 
  since 
  their 
  formation. 
  Among 
  many 
  good 
  examples 
  of 
  fault 
  

   scarps 
  in 
  homogeneous 
  rocks 
  are 
  those 
  on 
  the 
  west 
  sides 
  of 
  Moon, 
  

   Kelm, 
  and 
  Chase 
  mountains, 
  while 
  tilted 
  fault 
  blocks 
  little 
  affected 
  

   by 
  erosion 
  are 
  those 
  of 
  Moon, 
  Birch, 
  Crane 
  and 
  Huckleberry 
  

   mountains. 
  

  

  Little-Crane-Huckleberry 
  mountain 
  faults. 
  The 
  structural 
  rela- 
  

   tions 
  shown 
  by 
  these 
  three 
  mountain 
  masses 
  are 
  truly 
  remarkable 
  

   and 
  the 
  faults 
  are 
  the 
  most 
  interesting 
  within 
  the 
  quadrangle. 
  The 
  

   deep, 
  narrow 
  rift 
  between 
  Huckleberry 
  and 
  Crane 
  mountains 
  was 
  

   carefully 
  examined 
  and, 
  judging 
  by 
  the 
  frequency 
  of 
  outcrops, 
  it 
  is 
  

   quite 
  certain 
  that 
  a 
  narrow 
  belt 
  of 
  Grenville 
  separates 
  the 
  mountain 
  

   masses 
  as 
  shown 
  on 
  the 
  map. 
  A 
  narrow 
  valley 
  of 
  Grenville, 
  chiefly 
  

   limestone, 
  with 
  almost 
  continuous 
  outcrops 
  separates 
  Crane 
  moun- 
  

   tain 
  from 
  the 
  granite 
  ridge 
  just 
  south. 
  Likewise 
  there 
  is 
  a 
  valley 
  of 
  

   Grenville, 
  chiefly 
  limestone, 
  immediately 
  to 
  the 
  south 
  of 
  the 
  granite 
  

   ridge 
  (Little 
  mountain 
  and 
  its 
  westward 
  extension). 
  

  

  In 
  each 
  case 
  the 
  mountain 
  mass 
  of 
  igneous 
  rock 
  presents 
  a 
  

   high 
  and 
  very 
  steep 
  to 
  almost 
  precipitous 
  wall 
  on 
  the 
  south 
  side, 
  

   and 
  in 
  each 
  case 
  the 
  belt 
  of 
  Grenville 
  comes 
  abruptly 
  against 
  the 
  

   igneous 
  rock 
  wall. 
  A 
  slight 
  exception 
  to 
  the 
  latter 
  statement 
  is 
  

   along 
  the 
  southwestern 
  base 
  of 
  Crane 
  mountain 
  where 
  a 
  small 
  

   belt 
  of 
  syenite 
  intervenes 
  between 
  the 
  Grenville 
  and 
  the 
  high 
  

   mountain 
  mass. 
  Almost 
  invariably 
  the 
  rocks 
  of 
  the 
  Grenville 
  belts 
  

   dip 
  at 
  high 
  angles 
  downward 
  and 
  against 
  the 
  faults. 
  The 
  great 
  

  

  