266 THE IRON ORE DISTRICT OF EAST TEXAS. 



1 . Gray sandy soil 18 inches. 



2. Fragments and bowlders of iron sandstone 1 foot. 



3. Orange sand, upper bed, about 15 feet. 



4. Orange sandy loam 5 feet. 



5. Gray sandy soil or clay drift in road bed 6 feet. 



6. Lower bed of orange sand, changing at base to orange loam 10 feet. 



1. Gray plastic clay to bed of stream 15 feet. 



RELATION OF STRATA. 



In the northeastern portion of this county, the relation is similar (being a 

 continuation) to the section in northwestern Panola, from No. 1 to the lig- 

 nite, No. 1 8, the wavy laminated and buff crumbly iron ore excepted, as noted 

 in the description of that locality. These, if ever deposited, were eroded be- 

 fore the deposition of the iron sandstone and the overlying iron pebble con- 

 glomerate. 



In the central portion of the county, as at Millville, the sand underlying 

 the iron series becomes distinctly typical orange sand in the upper part of the 

 bed, but somewhat loamy at base, where it rests upon red clay. The absence 

 of fossils in the base, middle, and upper part ot the bed indicates that it was 

 local drift in agitated water. The Eocene fossils, Cardita planicosta, etc., in 

 the thin overlying stratum of iron sandstone two and one-quarter inches, in- 

 dicate a period of more quiet water. 



In the southern part of the county the sand bed is replaced by orange 

 loam, which is f ossiferous, containing Eocene fossils only in the upper por- 

 tion at and near the line of contact with the overlying buff crumbly iron ore. 



The parting of recemented angular fragments of iron sandstone and iron 

 pebbles derived from the summit capping of the ridges, now found between 

 the layers of greensand marl in Stevens Branch, near Sulphur Spring, is con- 

 firmatory evidence of the greensand marl having been deposited after the 

 deposition of the iron ore which caps the ridges. 



The fault in the lignitic micaceous sandy shale at Sulphur Spring indicates 

 that the disturbance which produced it was of course after its deposition. 



The tumbled bowlders of iron pebble conglomerate near by, as well as the 

 disturbed fossiliferous orange loam in front of L. D. Stevens' residence, indi- 

 cate that the disturbance was after the deposition of the iron ore. 



In the upper exposure of the greensand marl, on Stevens Branch, near Sul- 

 phur Spring, are pressure cracks, having the direction east 10° to 15° north, 

 and west 10° to 15° south. There is no reason to doubt that these were 

 made at the time of the disturbance, as they are within half a mile of it. If 

 we accept the Miocene hypothesis of the calcareous greensand shell marl, the 

 disturbance must have occurred after the deposition of the Miocene strata, or 

 at least a portion of it. 



