Geological Hisforij of the Czark Uplift — Broadhead. 11 
pying the summit on the north side. Passing northward from 
the river we find that in 12 miles these strata with the over- 
lying Trenton and Devonian have disappeared and are replaced 
with those of the lower Carboniferous. The general surface 
being about the same elevation on the south side would indi- 
cate a dip northward. We thus know we are on the confines 
of the Ozark uplift. 
A few miles below Glasgow an anticlinal brings the Chou- 
teau limestone to view, while the strata a few miles below and a 
few miles above belong to upper members of the Lower Car- 
boniferous, indicating an upthrow of probably 200 feet. 
Near Glasgow the Lower Coal Measures are at the base of 
the bluffs and continue so for a long distance up stream. At 
Miami, Saline county, nearly 100 feet of Lower Carboniferous 
beds appear in the bluffs, while on the north side the Lower 
Coal Measures are the lowest strata. 
At Sedalia the surface rocks are Lower Carboniferous (near 
the base) and on Muddy creek, west, we find the First Magne- 
sian limestone soon replaced by the upper members of the 
Lower Carboniferous and the Coal Measures. South of Sedalia 
are only found the Magnesian limestone series and in the north- 
east part of Cedar county they are the surface rocks while the 
Second Magnesian limestone is the lowest seen at Dunnegan's 
Mill, east of Stockton. On Cedar creek, west, the Keokuk is 
the bed rock. We therefore knoAV that Marshall, Sedalia and 
Stockton must lie near the break of the great monoclinal on 
the west. All along this line the Coal Measures are only a few 
miles west, separated by the intervening Keokuk outcrops from 
the Chouteau or the Magne-^iian limestones lying eastward. 
Westwardly the Coal Measures extend into Kansas and then 
dip beneath the Permian and the latter beneath the Cretaceous 
as we ascend towards the mountains. 
The southern foot of the Ozark uplift is probably near the 
Arkansas river. The Ozark plateau probably dates the begin- 
ing of its uplift in the early Carboniferous, or while the Chou- 
teau beds were being deposited, and continued during the 
Burlington period; and these rocks in many places have been 
deposited directly upon the Magnesian limestones but were 
soon eroded. This is shown by occasional local beds around 
the margin of the great uplift. 
