Apeil 2, 1909] 



SCIENCE 



557 



The locality at which the Little Missouri was 

 tapped, is in the big bend thirty miles northwest 

 of Bele Fourche. Its features are well shown on 

 the Aladdin quadrangle of the U. S. Geological 

 Survey. The former channel is now a flat-bot- 

 tomed gap through the divide about two miles 

 long and known as Stoneville Flat. To the north 

 it coalesces with the present Little Missouri 

 Valley, while to the south it ends in a cliff of 

 shale eighty feet high descending to the present 

 Belle Fourche River. 



At the 214th meeting of the society, held on 

 Wednesday, February 10, under informal com- 

 munications, Dr. J. W. Spencer presented briefly 

 some " Notes on Borings in the Vicinity of Whirl- 

 pool Eapids." 



Regular Program 

 The Pleistocene Phenomena of Southeastern Wis- 

 consin: Wm. C. Alden. 



This paper is based upon" detailed surveys of 

 an area of about 8,600 square miles south of 

 latitude 44° N., made under the direction of Dr. 

 T. C. Chamberlin. Outside the terminal moraines 

 of the Wisconsin ice sheet is a deposit of drift 

 regarded as of Illinoian age. The composition of 

 the drift and trend of striae show that the direc- 

 tion of ice movement was, in general, westerly to 

 the limit of the drift. The average estimated 

 thickness over 470 square miles of this area is 

 45 feet. Very compact reddish till and contorted 

 laminated clays exposed at intervals on the shore 

 of Lake Michigan at the base of the bluff are 

 correlated with this stage of glaciation. 



Some, at least, of the vegetal deposits pene- 

 trated by wells at many places throughout the 

 area of Wisconsin drift probably represent the 

 Peorian interval of glaciation. To this horizon 

 also may belong the logs and stumps observed 

 by Dr. J. W. Goldthwait near Manitowoc and 

 Two Rivers, Wis. One stump was found still 

 rooted in dense reddish clay provisionally classed 

 with the Illinoian deposits. 



The Green Bay, Lake Michigan and Delavan 

 lobes of the Late Wisconsin ice sheet are shown 

 to have been contemporaneous in their maximum 

 extension. Estimated average thickness of drift 

 in the terminal moraine of the Green Bay Glacier 

 at the south end of the lobe is 119 feet (this 

 includes older drift) . Along the west side, where 

 no earlier drift is known, the thickness is 61 to 

 77 feet. The estimated average thickness over 

 1,611 square miles of the ground moraine, in- 

 eluding recessional moraines, is 71.4 feet. Seven- 



teen hundred and fifty drumlins of good form 

 occur in the area examined. Evidence is found 

 that some were formed when the ice reached only 

 to one of the inner moraines. Eskers were formed 

 at or near the base of the ice and the esker-form- 

 ing streams were controlled by the configuration 

 of the drift surface. Direction of movement in 

 the adjacent parts of the two glaciers was almost 

 opposite. The interlobate moraine is 100 to 300 

 feet high, the relief generally being entirely of 

 drift. Drift of the Lake Michigan glacier esti- 

 mated as 100 to 150 feet thick at the south, 160 

 feet at the north and 45 feet midway between. 

 Recessional moraines are well marked. 



A readvance of the Lake Michigan glacier cov- 

 ered the moraines east of the Milwaukee River 

 with a deposit of red till southward to Milwaukee. 

 Between Sheboygan and Plymouth this extended 

 14 miles west of the lake shore. The estimated 

 average thickness of this deposit is 34 feet. In 

 Sheboygan and Manitowoc counties there is a 

 well-marked terminal moraine of red till over- 

 lapping the earlier recessional and interlobate 

 moraines. A similar deposit of red till bordering 

 Lake Winnebago indicates a readvance of the 

 Green Bay glacier to the south line of Fond du 

 Lac Township. This readvance is believed to have 

 occurred at the Glenwood stage of Lake Chicago. 

 There is a faint development of the Glenwood 

 beach on the red clay formed when the ice again 

 retreated. This is traceable north through She- 

 boygan County. In southern Sheboygan County 

 slight traces of a beach occur at the Calumet level. 

 Traces of the Toleston beach occur in Kenosha 

 County, but this was mostly obliterated during 

 the formation of the Nipissing shore, which is 

 strongly marked by cliffs and terraces about 14 

 feet above Lake Michigan. The Algonquin beach 

 is not distinguishable, possibly it is identical with 

 the Toleston shore. As shown by Goldthwait, 

 there has been little or no deformation of the old 

 shore lines in this area. Filling in the lower part 

 of Milwaukee River valley, consisting of marsh 

 deposits and alluvium extending 50 feet below the 

 level of the lake, indicate that at some time fol- 

 lowing the Glenwood stage and deposition of the 

 red till the lake waters stood considerably below 

 their present elevation. 



Clinton Iron Ores in the Birmingham District, 



Alabama: Ernest F. Bitbchabd. 



The Clinton formation lies on the flanks of a 

 non-symmetrical anticlinal valley, extending north- 

 east and southwest for about fifty miles, with the 

 city of Birmingham near the middle. Only on 



