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THH GHOLOGICAL

NATURAL HISTORY SURVEY

OF MINNESOTA.

The Twenty-second Annual Report, for the Year 1893.

oe ag
g | 35
N.. HoH. WINCHELL, 72 |

State Geologist.

MINNEAPOLIS:
HARRISON & SMITH, STATE PRINTERS.
1894.

THE BOARD OF REGENTS

OF THE
UNIVERSITY OF MINNESOTA.

HON. STEPHEN MAHONEY, Minneapolis..............-: .....-2-0e-- 1895
Hon. SIDNEY M. Own, Minneapolis: c7-. 2-73.20 sck- <a eee 1895
Hon. Jonn. LIND; New) Wilms: $5.0). sje%ic.c os tn ene ores ee eee 1896
HON, JOHN: S. PILLSBURY; Minneapolis'=. :...<0-.0~. . £2: ose ee 1896
HON: "OZORA P.. STEARNS, Duluth - 22.2. Peat oak. ve oe ee 1897
HON. WILLIAM -LIGGETT; Bens0n%. 34:24 ascents oblne e eeee 1897
HON. JOEL P.: HEATWOLE, Northfield...) 52-2-5::. 252-5 1897
HON. GREENETAF CLARK, St. Paul... 1.2.3. i842 02. ces oe ee 1898
Hon: CusHMAN K. DAVIs, St..Paul...%.¢ dxcw's deo eo ee eee 1898
Hon. KNUTE NELSON, Governor of the State................. Ex-officio
Hon. W. W. PENDERGAST, Supt. of Public Instruction ...... Ex-officio
Dr. Cyrus NORTHROP, President of the University .......... Ex-officio
oS OFFICERS OF THE BOARD.

HON. JOHNS. PILISBUR Yoiiide ste oe ee ay bd Oo hel ee President
AON MSE ITAL s 2 Snags Oo re nt doe mee ica wal atin Recording Secretary
PRESIDENT CYRUS NORTHROP......... gee feta Corresponding Secretary
JORRPH the AVA REL, sav ccow caer con ties tenes yxy o.eeiy CREO nee Treasurer

ADDRESS.

MINNEAPOLIS, Minn., Aug. 1, 1894.
To the President of the Board of Regents:

DEAR SiR—I have the honor to offer herewith the twenty-
second annual report of the Geological and Natural History
Survey of Minnesota. It embraces preliminary field reports
on a large amount of work, contributed by the various assist-
ants who were engaged on the survey during the season of
1895. It also contains lists of additions to the library and to

the museum.
Respectfully submitted,

N. H. WINCHELL,
State Geologist and Curator of the General Museum.

GEOLOGICAL CORPS.

L. A. OGAARD...............- SURVEYOR AND DRAUGHTSMAN

SPECIAL ASSISTANTS IN 18958.

Paleontology.

E. O. ULRICH, J. M. CLARKE,
W. H. SCOFIELD.

Field geology and topography, in charge of parties.

J... E¥ "Bopp, G. E. CULVER,
J. E. SPURR. A. H. ELFTMAN,
A. D. MEEDS, H. B. AYRES,

CP) BERKEx

General assistants.

A. N. WINCHELL, EK. R. BARTON,
H. B. HOVLAND, H. C. CAREL,
H. E. WHITE, R. P. JOHNSON,

R. M. WHEELER.

CONTENTS.

PAGE

Is so LITTER Veh ps 2 9 3 10S 0 ge aa Se Aas ne J

II. List of rock samples collected to illustrate the notes
BN Ae MEIN EVEN gee 0s cette cin neg. ue mpeg aun 6 wt ee 5

IlJ. Preliminary report of field work during 1893 in north-
eastern Minnesota, chiefly relating to the glacial

deity WARREN CUPEHAMS. 6.0 2o5 0. selec a wee aoe 18
PELCAS NOX AIMED scat se seis crate mickeene tors ovate see toceot urine uasstaiavate 19
MAD IHTBO ACCOMIPUSHEG. ac ss 5 3. <a se eiis 015% thes'nelut'as 19
Sketch of results of geological work.................. 26
IV. Preliminary report of field work during 1893 in north-
eastern Minnesota. By U.S. GRANT.............. 67
V. List of rock samples collected in 1893. By U.S.
BEN Ngee see Sais ee AE ys cc WE arta ee vine od oretnic o. 8 79
VI. List of rock samples collected in 1893. By A. D.
[TED Soe oe gaa A ee ee eS Pe 87
VII. Preliminary report of a reconnoissance in northwest-
ern Minnesota during 1898. By J. E. TopD......
ARON UVic 1 ia Ste er is nia hs lalate wisn n'a ee iele aw eisineis «sg 90
Summary of principal results........ ea Satan chosen 99
VIII. Notes on the geology of Itasca county, Minnesota.
ee Mee Ps MOL Babee, 5 as a aa Soe eace nies. aldcwlie’s + elas’ o Mele 97
WEL PPOUICDIGM opriape > 2 ode oer ciate elciore nies) oats wai chas Testis. 9Q7
SE OVE MONTE EDV fees or PEM a eciaieye aatats a! aie’ Sialelusn ais e[eie-arelocds 98
ROCIE BYSUCTIS: OUSOLVCU 1 .oc1> « buns «<0 sis tiers ace ore tee e 102
SIAC AMMNCHOMERA Seu oe koko yee «sce ce Ue nes 111
IX. Preliminary report of field work done in 1893. By
Spel DES] S TE 1018s Pi SEA eae en Rd Anes Se ES 115
EGER ATN Soe AG een ca gh tee eis cs tect wa ss ae nee s 116
CET AAPG ters ee Sep iarclecice Sxth ba oie ein dis she aren, 9 Sido ssaYorn 118
Salient points in the geology......................5. 119
X. List of rock samples collected in 1898. By J. E.
SLE ORR Te eet BARNES MALTS Nn yee ER ee Oe On! ee ane 125
XI. Preliminary report of levelling party. By C. P
RSPR LATO Ng s oe nae aor Steck ob sites WR ates olla’ s Sibel che Bioae w wle eye ele 134
XII. Preliminary report of field work during 1893 in north-
eastern Minnesota. By A. H. ELFTMAN.......... 141
General reper ol, HELV WOPKs = 5.5.0 <ece << k= sp winlee = Sn 141
Geological notes on northeastern Minnesota......... 150
XIII. List of rock samples collected in 18938. By A. H.
Eg PWEER AON crs cur) cioys/ orci eels asia wate stars.b’s sPES « wlee Nee © 181
PV ONIGSEUMD AGGIMONS 2)... e ues acess asic cece rcen ones 190
XV. Additions to the library since the report of 1892..... 198

XVI. The exhibit of the Survey at the Columbian Expo-
aCe PSN FEL, WAIN CERI ite So a scca ss vise p eos 201

PE
Pr

PL.

Pi:
Pip

rig
Il.

wel GO

ILLUSTRATIONS.

PAGE
Sections of quartzyte blocks, showing mode of

change of color. ...: 4.0.5.0... 3s seen 102

Hand specimen of ore-bearing rock, T. 56-24,
showing the irregular banding seen in cross

SOCTIONS, . .\ ws Gn bop -chiatgn Be o's k's oo os 1038
Showing stratigraphic relations at the falls of

Prairie river. ....0.2 -f2.iies. «ccs ce ® Se - = 105

FACING

PAGE

Map of the glacial geology of northern Minnesota 19

enaeeveicvecee ovens sets eps es gio. e 2 82 66 2 oS ©1590 @ Fe eee

Fig.1. Section on the D. & I R. R. R. in the
north part of sec. 1, T. 54, R. 12, 3 miles
northwest of Highland station.

Fig. 2. Section on the D. & I. R. R. R., in the
south part of the S W. + of sec. 23, T. 55, R. 12,
4+ to ? mile north of Thomas siding.

Fig. 3. Section on the D. & I. R. R. R., in the
southeastern part of sec. 15, T. 55, R. 12, 25
miles southeast of Cloquet River station.

Fig. 4. Section of part of the west side of the
Biwabik Iron mine, Oct. 18, 18938; showing in
the basal part of the drift two large masses of
the red iron ore whick were glacially uplifted .
and probably transported very short distances.

Section across the Mesabi range................ 120

. Two profiles across Cook county, from Brulé

lake and from Grand Marais N. N. W. to the
International boundary...............-.-.00e8 138
Map of the west central part of Lake county.... 150
Fig. 1. Geological map of the western end of
Birch lake and adjoining country southward.
Fig. 2. Cross section from Moose lake to Snow-
bank lake.

160

-:
SUMMARY STATEMENT.

An effort was made in 1893 to finish that amount of field-work
necessary to warrant the preparation of the final report and
maps of that portion of the state remaining unpublished. A\l-
though there are still many unknown elements in the geology
of the northern part of the state, and some considerable tracts,
remote from routes of travel, some of which have not been
‘‘subdivided” by the township survey of the United States gov-
ernment, which the parties of the geological survey have not
been able to visit and map, yet it is thought best to close up the
active work in the field and to enter upon the preparation of
the last volume of the final report. It was with an earnest de-
sire to round out the present survey with what might be called a
final report, showing its completed results in systematic rela-
tions, within the reasonable term of a single administration,
that the writer, four years ago, volunteered to pledge the com-
pletion of the field-work for the sum of twenty-five thousand
dollars. This was stated to the appropriation committees of
the Legislature of 1891. Fifteen thousand dollars were appro-
priated by that Legislature. The last Legislature (1893) ap-
propriated ten thousand dollars under similar representations.
Although the full sum of twenty-five thousand dollars has not
yet been expended on the field-work, yet so much has been done
that nearly all the remaining plates. which will represent the
geology in the final report, can be drawn. There will be need
yet of special examination in some difficult and some important
areas, where the opportunities of the past have not been favor-
able to entirely and satisfactorily understand the geological
structure. Practically, however, the campaign of 1893 may be
said to have finished the field-work. The rest of the time to be
devoted to this work by the writer will be given, as now con-
templated, to the preparation of the last final volume, with the
necessary accompanying maps.

ae
, 4

2 TWENTY-SECOND ANNUAL REPORT

During the last season parties were in the field under the fol-
lowing assistants:

Prof. J. E. Todd, in the northwestern portion of the state,
north and east of Red lake.

Prof. G. E. Culver, in Itasca county.

Mr. Warren Upham, in Aitkin and Cass counties.

Mr. J. E. Spurr, on the Mesabi range and southward in St.
Louis county.

Mr. A. D. Meeds, on the Magabis range and southward in St.
Louis county.

Mr. A. H. Elftman, on the Mesabi range and southward in
Lake county.

Dr. U.S. Grant, on the Mesabi range and southward in Cook
county.

Mr. C. P. Berkey, from Grand Marais northward, in Cook
county, and in co-operation with Dr. Grant.

The writer also was in the field in different places. but chiefly
in Cook county. Mr. H. B. Ayres began work in Carlton county,
but was interrupted by sickness and afterward by other engage-
ments, and accomplished but little. It is planned that he will
finish his allotment of work in Carlton county the coming
season.

In view of the proposed final mapping of the rest of the state
it was deemed highly desirable to obtain such hypsometric data
as would warrant the approximate drawing of contour lines in
the manner shown on the final plates already published in vol-
umes I and Il. Each party was furnished with the necessary
instructions and apparatus for platting these lines cn the field
maps which they carried, while at the same time a continuous
hourly reading of a mercurial barometer was recorded at
‘‘Mesaba* station,’ by means of which the simultaneous aneroid
readings of the different parties could be corrected and reduced
to a uniform basis, and referred to the sea level. In this way
a large mass of data was obtained which, when corrected and
platted, will result.in contour lines, 50 feet separate, over a large
area in the northern part of the state. This will give an ex-
pression of a preliminary topographical reconnaissance, and
will serve as an introduction to the topographical map which it
is hoped may yet be constructed. At the same time it is an in-

* There having been great diversity in the spelling of this word, the matter was
brought before the United States Board of Geographical Names, of which the Superin-
tendent of the Coast ana Geodetic Survey is president. On consideration of the vari-
ous spellings, numbering about half a dozen, it was decided by the Board that the
correct orthography is Mesabi.

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STATE GEOLOGIST. 3

dispensable aid in the understanding of the geological maps
and descriptions. Simultaneously with this system of hypso-
metric readings, a line of levels was run by means of a survey-
or’s level by Mr. L. A. Ogaard, in company with Mr. Berkey,
from Grand Marais across the country to the International
boundary, designed to cross what was supposed to be some of
the highest land in the state. Many hills, lakes and streams
were thus accurately ascertained. This series of levels was
widened out to the right or left whenever opportunity occurred
so as to include important adjoining points. The highest point
found was at the summit of the Misquah hills, 2,230 feet above
tide, in the N. E. part of sec. 35, town. 64, range 2 W. The re-
gion about is made up of the well-known ‘‘red-rock.” This
range of hills, inits extension some miles further east and west,
has nearly as great altitude. The examinations of the season
have also demonstrated that the actual water-divide from this
place southwestward to Duluth is essentially composed of the
same rock, variously mingled with the gabbro of the Mesabi
range. The general results of some of these examinations are
given in the accompanying reports of the assistants mentioned.
More of the details and the final conclusions will be set forth
in the final report.

While the accompanying reports give, in the main, the gen-
eral results of the various field parties, in the words of the as-
sistants themselves, that of Mr. Spurr, who was occupied on
the productive portion of the Mesabi range, in the vicinity of
Biwabik, McKinley and Virginia, and who has supplemented
his field-work by a careful investigation in the laboratory,
reaching highly interesting and important results as to the ori-
gin of the ores of the range, has been published as a separate doc-
ument (Bulletin X). The 2ist report of the survey has also been
issued and distributed. Volume III, of the final report, is still
in press. Only a part of the paleontoiogy of the Lower Silurian
can be included in the volume. The gasteropods and cephalo-
pods, which the volume had been intended to cover, and for
which preliminary contracts had been executed, have to be
omitted These chapters, however, will be published at some
future date, as now planned, and probably as bulletins of the
survey. Of the volume, however, the following chapters were
issued since the last report:

Chapter VJ. The Lower Silurian Lamellibranchiata of Minnesota. By
E. O. Ulrich. Pp. 475-628, 8 plates. Published June 16, 1894.
Chapter VII. ‘The Lower Silurian Ostracoda of Minnesota. By £. O.
Ulrich. Pp, 629-693, 4 plates. Published July 24, 1894.
Other papers by members of the Minnesota geological corps

4 TWENTY. SECOND ANNUAL REPORT o.

have been published, as follows. elsewhere. These have a
bearing on the geology of the state and of the Northwest. Str
Volcanic Rovks in the Keewatin of Minnesota. U.S. Grant. Science, =
vol. xxiii, p. 17, Jan. 12, 1894. Bs ay
Note on the Keweenawan rocks of Grand Portage Island, north coastof ~~
Lake Superior. U.S. Grant. American Geologist, vol. xiii, pp.437-
439, June. 1894.
Epeirogenic Movements associated with Glaciation. Warren Upham.
American Journal of Science, III, vol. xlvi, pp. 114-121, Aug., 1893.
Altitude as the Cause of the Glacial Period. Waurren Upham. Science,
Aug. 11, 1893. :
Beltrami Island of Lake Agassiz. Wurren Upham. American Geologist,
vol. xi, pp. 423-425, June, 1893. Tey ae ae
Englacial Drift. Warren Upham. American Geologist, vol. xii, pp.36-43,
July, 1893. eee ye
Early Man in Mionesota. Warren Upham. Am. Geologist, vol. xiii, pp. Nie Wat
363, 364, May, 1894. f Rigied
Causes and Conditions of Glaciation. Warren Upham. Am. Geologist,
vol. xiv, pp. 12-20, July, 1894.
The Niagara Gorge as a Measure of the Postglacial period. Warren Up-
ham. Am. Geologist, vol. xiv, pp. 62-65, July, 1894. s
The Madison Type ot Drumlins. Warren Upham. Am. Geologist, vol.
xiv, pp. 69-83, with pl. iii, Aug., 1894. > apie
Evidences of the Derivation of the Kames, Eskers, and Moraines of the Ce
North American Ice-sheet chiefly from its Englacial Drift. Warren : :
Upham. Bulletin of the Geological Society of America, vol. v, pp- eS eae
71-86, Jan., 1894. a> here
The Succession of Pleistocene Formations in the Mississippi and Nelson. Bei?
river basins. JVarren Upham. Bulletin of the Geol. Soc.of America, —
vol. v, pp. 87-100, Jan., 1894.
How Old is the Earth? Warren Upham. Popular Science Monthly, vol.
xliv, pp. 153-163, Dec., 1893. me
Increase Allen Lapham. NV. H. Winchell. American Geologist, vol. xiii, —
pp. 1-38, Jan., 1894. i E
Pebbles of Clay in Stratified Gravel and Sand. WN. H. Winchell. Glacial-—
ists’ Magazine, vol. i, pp. 171-174, March, 1894.
Note on Cretaceous in northern Minnesota. H. V. Winchell. American
Geologist, vol. xii, pp. 220-223, Oct., 1893. ; ons
Additional Facts about Nicollet. H. V. Winchell. Am. Geologist, vol. =
xiii, pp. 126-128, Feb., 1894. me
A Bit of Iron Range History. H. V. Winchell. Am. Geologist, vol. xiii, 2
pp. 164-170, March, 1894. eS
The Discovery of Mineral Deposits in the Lake Superior region. 4. V. x
Winchell. Proc. Lake Superior Mining Inst., vol. ii, 1894. ar
False Bedding in Stratified Drift Deposits. J. EB. Spurr. Am. Geologist,
vol. xiii, pp. 43-47, Jan., 1894. ‘ a ES
Oscillation and Single Current Ripple-marks. J. #. Spurr. Am. Geolow
gist, vol. xiii, pp. 201-206, March, 1894. Baie
The Iron Ores of the Mesabi Range. J. E..Spurr. Am. Geoligist, vol.
xiii, pp. 335-345, pl. viii. May, 1894. to4) =
The Stratigraphic Position of the Thomson Slates. J. E. Spurr. Amer.
Jour. Sci., 111, vol. xlviii, pp. 159-166, Aug., 1894. ie

y Ie

LIST OF ROCK SAMPLES COLLECTED TO ILLUS-
TRATE THE NOTES OF N. H. WINCHELL, 1893.

1786. Coarse diabase, from a branching conspicuous dike,
or bleb, which crosses, in part at least, the town site of Ely.
It is seen on the highest portion of the town, cutting the boul-
dery graywacke, near the Catholic church. .

1787. Amygdules, or pipe-like tubes, in the boulders or
bombs of the agglomerate at Ely, filled with silica which ap-
pears to be ‘‘chalcedonic” or minutely granular. This new
feature is found sparsely in the rock toward the southwest
from the cut at the railroad already described. (Specimen lost).

1788. The diabasic rock mentioned under 1786 appears south-
westward from the railroad cut, toward the Lockhart property

_ (at Ely), and where it abuts against a bouldery mass of the

graywacke or agglomerate, its grain and substance seem to
enter the bouldery mass, at the same time becoming finer, and
to surround the bombs, forming the dark-green scale which
envelops them. This number, 1788, is a sample of the massive
rock which enters, apparently, the graywacke and surrounds
the boulder-like masses.

1789. An irregular, irruptive, siliceous rock, a kind of
quartz porphyry. appearing in the midst of the greenstone on
a knob about three-fourths mile west of the depot at Ely.

1790. Finely porphyritic or amygdaloidal diabase, like 1788,
the amygdules (?) filled with a dark green mineral (chlorite ”),
north from the Chandler mine, at Ely.

1791. In the conglomeritic portions of this greenstone, par-
ticularly in the matrix surrounding the boulders, is coarse
Silica, with calcite crystals, mingled in which are also isolated
pieces of some green shale or scale, seen north from the Chan-
dler mine,

1792. In some places the foregoing minerals (silica and
calcite) become abundant, though very fine-grained, forming

6 TWENTY-SECOND ANNUAL REPORT

lenticular masses of siliceous marble, which stand vertical.
These are white, and from two to four inches thick and three
or four feet long.

1793. Basal conglomerate, from the bottom of the supposed
preglacial gorge, at Virginia. This is of ferruginous pebbles,
mingled with dust and dirt of the iron bearing rocks. It may
be of Cretaceous origin. It has a later infliltration of white
silica which now forms its principal cementing bond.

1794. Forms of taconyte, showing transition from rock to
ore, Moose mine near the line of separation from the Ohio,
Virginia.

1795. Forms of the ore, Lone Jack mine, Virginia.

1796. Dark, diabasic rock which blends with the gabbro as
if only a phase of the gabbro, at Duluth.

1797. Gabbro embracing small masses of augite- saenfed at
Duluth, and containing as a result, numerous crystals of ortho-
close as a constituent of itself.

1798. Siliceous pebbles or claystones from the Keewatin
schists or slates about amile and a half northeast of Otter
Creek station, at the highway north of the St. Paul & Duluth
railroad.

1799. Pebbles of disintegration from the gabbro at 1013
Michigan St.. Duluth.

1800. Diabasic structure in the gabbro, thin plagioclase
crystals lying parallel over large areas making a lath-shaped
marking when weathered; same place as the last.

1801. Gneissic structure in the gabbro (rather a dioryte),
taken at the point where the grand boulevard (running ap.
proximately on the upper beach) crosses a small creek back
from Rice’s point.

1802. Gabbro containing dark-green inclusions. Tnese
small dark-green masses are rather fine-grained and they seem
to have affected the gabbro surrounding them by disseminat-
ing an element which, entering among the gabbro elements,
has given rise to a red weathering feldspar and hornblende,
along with some epidote. These dark-green spots, with the
accompanying discoloration impart a noticeable spottedness to
the gabbro mass wherever they occur.

1808. A fine-grained rock from the gabbro near the dam
of the little creek where it is ponded above the grand boule-
vard, at Duluth.

1804. Ata point midway between the dam and the elevated
station of the elevated railroad, Duluth, is a large surface

STATE GEOLOGIST. 7

exposure of some old metamorphic rock, some of it being
brownish-red, and some of it gray. It is below the crest of
the gabbro range, and on the southern slope, but is embraced
within the general gabbro area. The red areas somewhat
embrace the gray or blue. This number represents the red
rock.

1805. Is the fine-grained gray rock. This is sometimes
apparently a conglomerate, holding boulders of quartz and of
granite, but in general it is a uniform rock. In some cases the
red rock shades into the blue, even on the surface.

1806. Both of the above sometimes are amygdaloidal—at
least are flecked with rounded dark-green spots about which
are reddened areas resembling the inclusions in the gabbro,
(1802).

1807. Samples from the sedimentary patches embraced in
the amygdaloidal parts at Cow Tongue point, north shore of
lake Superior.

1808. Pebbles from the hard fine grained, gray sedimenta-
ries, got on the beach one mile west of Brulériver. They vary
from blue to reddish, and one is white.

1809. Red rock pebble, from the same beach. These are
usually amygdaloidal, and sometimes also porphyritic.

1810. Green doleritic trap pebbles from the same beach.
These are very rare, although the rock outcropping on the
shore, at all the points, consists of such trap.

1811. From the vertical cliff forming the west shore of
Sickle bay—a rather fine-grained gabbro.

1812. Showing contact of this gabbro with a very fine-
grained black rock, from a pebble on the beach.

18138. Poikilitic gabbro, from the west side of Double bay,
at the point. The pyroxene shows its own sheen in the sun-
light over large crystal surfaces.

1814. Gabbro from the hill range at Double bay, at the west
end of the near hills.

1814A. White-weathering lumps and patches in 1814.

1815. In descending the hill again we encountered a slightly
different phase, being very coarse with dark crystals of pyrox-
ene and light-weathering large crystals of same plagioclase.

1816. Coarsely rough gabbro, at one mile east of Cannon
Ball bay.

1817. Coarse gabbro, with poikilitic crystals of pyroxene,
at a point two miles west of the west side of Red Rock bay.

8 TWENTY-SECOND ANNUAL REPORT

1818. From the southern (basaltic) dike of the two trap
dikes cutting the ‘‘red rock” on the eastern side of Red Rock
bay.

1819. From the northern (non-basaltic) of the two dikes cut-
ting the ‘‘red rock,” at the same place, two feet from the’ con-
tact with the other.

1820. Of the northern dike at the contact with the southern.
These dikes are nearly parallel (east and west), but interfere
with each other, the northern dike being the later.

1821. From a branching dike of diabase, or ‘‘ black trap,”
at the extremity of Red Rock point. It has a pitted surface,
from the decay and removal of some soft mineral.

1822. Quartz porphyry, Red Rock point.

1823. Sample from low rocky knob rising but little above
the water, near the shore, within the bay next east of Red
Rock point, but near Red Rock point, apparently underlying
all the quartz porphyry.

1824. A curious, shaly-looking rock within the bay next east
from Red Rock point, cut by conspicuous dikes that appear to
be of the same age as those that cut the quartz porphyry.

1825. The same, having a spotted appearance.

1826. Amygdaloidal phases of 1824.

1826A. Agates from 1826.

1827. A metamorphic quartzyte, evidently some of the
Wauswaugoning quartzyte, from the southern face of Mt. Jose-
phine, about 500 feet above the lake.

1828. Basic irruptive rock concerned in the metamorphism

of 1827.

1829. Average rock of the top of Mt. Josephine.

1830. ‘‘Red rock,” kind of quartz porphyry, from a hill
northwestward from Mt. Josephine, where it forms an irreg-
ular patch elongated about east and west, visible on the south-
ern slope of the gabbro range.

1831. Conglomerate, from the east side of Grand Portage
island.

1832. Darker and finer-grained sandstone(?), same place.

1833. From the very top of 1832, where it is in contact with |

an overlying trap sill.

1834. <A peculiar, nearly black, amygdaloidal rock found on
the very top of the island and extending westward gradually
descending to the water level.

1834A. A lot of balls from 1834.

STATE GEOLOGIST. 8)

1884B. Series of red pebbles, from the beach of Grand Port-
age island. .

1834C. Fine red granite, porphyritic with quartz, from a
hill rising about 600 feet above the lake, about a mile and a
half from Grand Portage, on the west of the Grand Portage
trail. It is on one of the highest cliffs on the southern side of
the hill, but forms only a small part of the hill, which consists
rather of the gabbro of the region, being a part of the great
dike range of which Mt. Josephine is a spur.

1835. Same contorted slate, from the low hill of slate, cut by
numerous dikes, which rises near the lake at Grand Portage.

1836. A possible organic impression, from the slates of 1835.

1837. Upper portion of the Wauswaugoning quartzyte. Itis
gray, somewhat colored like the slates, spotted with light red,
pink, or even green; from the foot of Mt. Josephine at the
head of Wauswaugoning bay.

1838. The same, sub-crystalline, fine-grained.

1839. The same, having the form of quartz porphyry, ap-
pearing in patches in 1838, and also largely.

1840. The same, spotted with red and green.

1841. Plumbaginous quartzyte, from the old graphite mine
on Pigeon point.

1841A. Spotted gray quartzyte, from the beach near the
head of Morrison bay.

1842. Atone-half mile west of Little Portage bay (i. e., where
Pigeon point is norrowest), the axis of Pigeon Point peninsula
is composed of a dark-greenish but spotted modified quartzyte,
the spots being coincident with or caused by poikilitic crystals
of some rock-making mineral, apparently some feldspar.

1843. Gabbro, extremity of Pigeon point.

1844. Red rock, near the extremity of Pigeon point.

1845. Modified Wauswaugoning quartzyte, from the knob
rising near the south shore of Pigeon point a little west of Lit-
tle Portage bay—a quartz keratophyre. according to Bayley.
This knob consists of various conditions of this quartzyte.

1846. Possible organic impressions in a limestone, septaria-
like mass, weathered from the slates on the south side of the
tongue which divides Pigeon bay into north and south arms.

1847. An amygdaloid with green fillings, at the eastern end
of the outer and eastern of the Lucille islands.

1848. Massive pyroxenic rock, apparently in form of a dike,
cutting 1847, same place. ;

10 | TWENTY-SECOND ANNUAL REPORT

1849. Porphyritic gabbro running diagonally, like a dike,
across the same island.

1850. Red rock attached to 1849.

1851. Ore, from the Susie Island shaft, Pigeon Point Silver
and Copper Mining company, an ill-starred enterprise inspired
by the late T. M. Newson.

1852. Quartzyte and black slate, showing contact of sedi-
mentary sequence in the shaft. It is apparent that while the
shaft started in hardened slate at the surface, the excavation
struck red quartzyte and finally red granite.

1853. Red granite from the bottom of the shaft.

1854. Black slate, at the Susie Island works, becoming
crystalline with orthoclase and turning red on weathering.

1855. Sample of dike forming a little point about one mile
west of the west point of Grand Portage bay.

1856. Amygdaloid cut by this dike.

1857. Amygdaloid, center of sec. 20, first point west of the
last.

1858. Supposed sedimentary material containing laumontite,
from the western side of Cow Tongue point.

1859. Red rock, not quartz porphyry, from the west side of -

Cow Tongue point.

1860. Quartz porphyry of the red rock series, on the S.
town line of 62-1 E., where the new road from Grand Marais
crosses it. This is also amygdaloidal, which is a new point in
the petrology of this series.

1861. Coarse poikilitic gabbro, from the hills next north of :

the Brulé lakes, on the Iron trail.

1862. Finely granitic red rock, on the portage south from
Misquah lake.

1863. Dark gray, or reddish-weathering fine-grained rock
holding porphyritic crystals of feldspar, from the north side
of Brulé lake at the portage north to Lost lake.

1864. Porphyritic orthoclase gabbro, S. W. 4 see. 13, T.
63-3 W., south shore of Brulé lake.

1865. A dark gray, rather fine-grained rock which is sup-
posed to be derived from the porphyry series, S. W.+ sec. 14,
T. 63-3 W. south shore of Brulé lake.

1866. Red rock porphyry. Probably S. E.4sec. 15, 63-3, W.

1867. Orthoclase gabbro, S. E. 4, S. W. 4, sec. 24, T.
63-3 W.

1868. Red rock forming the hill in W. 4, N. E.4, sec. 25,
T. 63-3 W. .

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STATE GEOLOGIST. 11

1869. Fine grained orthoclase gabbro, south side of the
island in N. E. 4, S. W. 4, sec. 24, 63-3 W.

1870. Peculiar gabbro, east end of the island, S. W.i, N.
HE. 4, N. E. 4, sec. 13, 63-3 W.

1871. Fine grained gray rock, with spots resembling
amygdules. No structure made out in this rock; eastern point
of the large island, N. H. 4, S. W. 4, sec. 18, T. 62-2 W.

1872. A phase of the same. These two specimens well
represent the rock of this point.

1873. Red rock. fine grained and dark colored, N. E. i, S.
E. 4, sec. 18, T. 63-2 W. This is the eastern end of a range of
red rock hills that lies on the south of Brulé lake in this ,;
section and S. 3, N. W. 4, sec. 17.

1874. Dark porphyry, intermediate between the gabbro
and the reddish porphyry (1863) seen about Brulé lake. South
side of a small lake in the N. E. 4, N. H. 4, sec. 17, T. 63-2 W.
The same is seen along the south shore + mile further east.

1876. Dark, compact, fine grained rock, with a tendency to
a reddish color. Small dark areas of crystalline material,
surrounded by a vein of red which grades into the rest of the
rock, are common, N. E. }, N. E. 4, sec. 20, 63-3 W.

1877. Quartz porphyry, with black groundmass, in which
are small quartzes and feldspars, the latter redish to flesh-
color, and frequently having the outer part redder than the
interior, N. E. 4, N. W. 4, sec. 20, T. 63-3 W.

1878. Quartz prophyry with dull red groundmass, small
quartzes and red feldspars, which latter are not usually very
distinct, as they are of about the same color as the ground
mass, N. W. 4, N. W. 4, sec. 20, T. 63-3 W.

1879. <‘‘Black rock,” so-called, on a small island in the N.
W. i, S. HE. 4, sec. 18, T. 63-3 W.

1880. Spotted phase of the same, at the western outlet of
Brulé lake, N. H. 4, S. W. 4, sec. 18, 63-3 W.

1881. Rather fine grained ‘‘pepper-and-salt” rock, in a low
ridge crossing the trail from Brulé lake, S. W. 4, N. W. 4, sec.
18, T. 63-3 W., apparently in form of a dike.

1882. Fine grained red rock, from the precipitous cliff on
the eastern side of the hill rising at the S. W. corner of sec.
8, T. 63-3 W.

1883. Hard “black rock,” N. E. 4, N. E. 4, sec. 17, 63-3 W.

1884. Red “black rock,” N. W.4, N. E. +, sec. 16, 63-3 W.

1885. Amygdaloid-like porphyry, from a reef-like island

»
12 TWENTY-SECOND ANNUAL REPORT

just off the eastern most point in S. E. 4. S. W. 4, sec. 10,63-3 |

W. The amygdaloidal spots are sometimes + inch in diameter.

1886. Black rock from the hills in the N. part of sec. 18, T.
63-3 W. at the west end of Brulé lake.

1887. A slaty fragment from the ‘‘black rock” forming a ‘
part of one of the hills in N. E. 4 sec. 18, 63-3 W.

1888. Black rock, apparently with fine quartz grains. Same
place as the last. .

1889. Pseud-amygdaloid in the black rock, at the Temper-
ance river outlet of Brulé lake.

1890. Apparently a coarse diabase, or a fine gabbro, possi-
bly a derivative of the black series, cut by veins of red granite.
Same place.

1891. Graphic granite, from veins and patches in the gabbro
cut on the spur of the railroad near Paulson’s camp.

1892. From an eighteen inch dike cuttiug the gabbro, seen
on the railroad about a mile east of Paulson’s camp.

1893. Fairsample of the iron ore at Paulson’s, sec. 28, 65-4W.

1894. Pyrite, thought to contain nickel. Paulson’s.

1895. An unknown mineral connected with the pyrite, from
the quartzyte at Paulson’s. This mineral is cinnamon colored.

1896. Average sample of an isolated ridge of Animikie
saparated by a range of greenstone from the main mass of the
Animikie, lying in S. W. + sec. 21, 65-4 W., near Paulson’s
camp.

1897. Some of the finest portion of a singular slate-and-
quartzyte breccia occurring in a low ridge by the railroad
(south side), at the peat swamp crossing, about 1 mile west of
the narrows of Gunflint lake.

1898. From the center of the conspicuous vertical dike which
cuts the trap hill at the west side of the outlet of South Fowl
lake.

1899. From the same dike from its contact with the trap
forming the hill.

1900. Fair sample of the gray trap of the hill, remote from
the dike.

1901. The trap near the dike, apparently changed to a
greater denseness through the action of the dike.

1902. Fine quartzose conglomerate, overlying the next, dip-
ping southward, toward the hill-range, from about the center
of the N. W. 1 of sec. 25, 64-4 E., southward from South Fowl
lake.

STATE GEOLOGIST. 13

1903. Lower portion of the conglomerate represented by
1902. These are each visibly about 18 feet thick, and grade
into each other. The upper mass resembles the finer portions
of the gritstone seen at the east end of Grand Portage island,
and the lower one is like the coarse quartz-pebbly conglome-
rate seen near Fond du Lac in the valley of the St. Louis river.

1904. From the bottom of the perpendicular escarpment
forming the top of the same hill. The hill rises about 350 feet
above the country immediately north. This represents the
top of the gritstone, and is similar to 1902. The gritstone has
a thickness of about 126 feet, although it cannot all be seen
exposed. ;

1905. From the top of the same hill, a non-descript rock
resembling some Keewatin.

1906. A fine-grained member of the gritstone, from an ex-
posure further east.

1907. Slate, south of the Millie mine, Iron Mountain, Mich.

1908. Limestone, ‘‘the limestone,” same place.

1909. ‘‘Potsdam sandstone,” unconformable over the lime-
stone, same place.

1910. Typical jaspilyte of the Chapin mine region.

1911. Ore of the Chapin mine region, with ‘‘carbonate”
interbedded.

1812. Rhodochrosite (?), Chapin mine ore dump.

1913. The conglomerate supposed to lie between the Millie
and the Chapin, from the Quinnesec ore dump. from an old pit.

1914. Same of the schistose and calcareous portions of the
greenstone, on the Wisconsin side, Lower Quinnesec falls,
Menominee river.

1915. Some of the massive, ditto. .

1916. Green schist, with quartz and carbonate of lime.

1917. Finely laminated, apparently sedimentary structure,
in the green schists on the Michigan side, Lower Quinnesec
falls.

1918. Coarsely crystalline, apparently gabbro-like rock
thrown out in the excavation for the channel for running logs,
Lower Quinnesec falls.

1919. ‘‘Actinolite-magnetite schist’ and hematite, from the
‘lower Huronian,”’ at a point in the first hill just south of the
Republic mine, Michigan. Structure dips N. about 75 deg.

1920. Quartzyte, supposed to belong below the last, a little
further south. The visible stratification here dips N. about
50 deg.

14 TWENTY SECOND ANNUAL REPORT

1921. Fine quartzose mica schist, in a narrow band visible
about 18 feet, running in the granite, a little further south.

1922. Fine mica schist holding quartz pebbles, at the base,
as supposed, of the ‘‘lower Huronian,” lying on a granite
which appears to be irruptive, and from which it is supposed
to have derived boulder masses, about half a mile further
south.

1923. Breccia of jaspilyte, cemented by dark jaspilyte, and
by iron, Republic mine.

1924. Quartzyte, from the Republic ridge, at the point
where the evident discordance occurs.

1925. From the same quartzyte, becoming sericitic, from
an old mining location on the opposite side of the lake.

1926. Garnetiferous mica schist. from the same side of the

lake but further west, a surface exposure thought to be from
the top of the ‘‘upper Huronian.”

1927. A much changed large dike of basic rock, running
puede! with the strata in the ‘‘upper Shasta at the rail-
road cut, west side of the lake.

1928. Conglomerate containing copper, Calumet and Hecla
mine.

1929. A boulder-like mass, containing a large amount of
copper, apparently a boulder of amygdaloid or other porous
rock which has received copper into its interstices, same place.

1930. ‘‘Shot copper,” originally an amygdaloidal fragment
of some eruptive rock embraced in the general conglomerate,

has been permeated by metallic copper from solution, same ~

place.

1931. String copper, with a little silver, from which the
associated boulders have been separated.

1932. Calcite crystals, containing interleaved copper; same
place.

1933. ‘Half breed”, i. e. mass of metalic copper containing
some silver, found under the stamps. Calumet and Hecla.

1934. ‘Baby ingot’ of metallic copper. Calumet and Hecla.

1935. Sandstone having a matrix of metallic copper. Calu-
met and Hecla.

1936. ‘‘Melaphyr” trap, taken from the Tamarac shaft, near —

the Calumet and Hecla mine, the most abundant rock a
through in the 3,000 ft. New shaft.

1937. Variation of this trap rock, with some epidote.

1938. Carbonate, supposed to be that from which the iron

STATE GEOLOGIST. 15

ore of the Palms mine (near Ironwood, Mich.), and of the Go-
gebic range in general, is derived. From near the Palms mine.

1939. Tufaceous material, in the ‘‘upper Huronian”’, inter-
bedded with the iron-bearing rocks. From the dump at the
Palms mine.

1940. The siliceous slate south of the Aurora mine, involved
in the granite, whether by irruptive contact or by sedimentary
non-conformity, is a point of difference.

1941. The granite here contacting.

1942. Some of the poikilitic, most coarsely cr aapalliets por-
tion of the gabbro at the first railroad cut (most westerly) near
Short Line park, on the St. Paul & Duluth R. R. From the
east end of the cut. Much of this rock at the first cut is
amygdaloidal, especially toward the western end of the cut,
and on the western face of the hill, and most of it is rather a
green trap or diabase, when not amygdaloidal.

1943. Very fine-grained, dense, olivinitic gabbro, weathers
greenish. From the second cut east of Short Line park, (on
the E. line of S. E. 4 sec. 33).

1944. The usual black irony belt in the gabbro hill at the
same place, visible on the west face of the hill.
1945. Coarse olivinitic, magnetited gabbro. Same place.

1946. Underlying coarse gabbro, same place.

1947, From veins, or seams, in 1946, same place.

1948. Highly blackened gabbro, from another cut further
east, probably in the east side of sec. 384. This is rather fine
grained but not observably magnetic. It constitutes but a
small part of the prevailing rock.

1949. From a detached amygdaloidal mass between the
depot and the river at Cloquet.

1950. Average type of the gabbro of the first (westerly) hill
range, in sec. 33, near Short Line park.

- 1951. Three samples showing the average amygdaloidal
structure in the same hill.

1952. One of the narrow amygdaloidal dikes cutting this
hill, with contact on the gabbro, same place.

1953. From a large dike running N. 15 deg. E., same place.

1954. Massive homogeneous, irruptive rock mingled with
the bombs and graywacke in the ‘‘greenstone formation” near
(but north from) the depot at Ely. (Specimen lost.)

1955. “Concretionary, rounded small masses, resembling
those figured on p. 318 of the 16th annual report, from the

16 TWENTY-SECOND ANNUAL REPORT

ambiguous greenstone at Ely, near the Catholic church. (Spec-
imen lost.)

1956. A breccia embracing some green fragments of the
schist.

1957. Sub-crystalline porodyte, or feldspathic quartzyte,
north side of Ely island, Vermilion lake. With the exception
of a little argillyte at the west end of this island the whole
north shore consists of rock of this kind.

1953. Apparently burnt jaspi'yte, from the mainland south-

east from Ely island. This appears as a black, slaty argillitic

jaspilyte, in the midst of porodyte, and runs at least one-fourth
mile, with the usual strike, standing nearly vertical, or dipping
85-90 deg. toward the north.

1959. Three pieces showing the south contact of this on the
porodyte. No effect, so far as can be seen, is produced on
either; but the porodyte simply becomes some finer and green-
er. We subsequently noted the same contact on the north side
of a jaspilyte belt, with the same result.

1960. Some squeezed masses of jaspilyte showing the
changed forms of pebbles of different colors. North side of
the north ridge, at Soudan.

1961. Apparently pebbles, pressed, enclosed in hematitic
jaspilyte, but on close examination they appear to be remnants
of reddish jaspilyte replaced otherwise by hematite.

1962. A form of the greenstone which appears on the north
slope of the ‘‘north ridge.” It has an approach toward
argillyte.

1963. <A black slaty jaspilyte is seen near the limonite local-
ity, where a large amount of limonite was taken out by the
Minnesota Iron company but not shipped, north from Soudan.
Is it carbonaceous ?

1964. Another coarse, siliceous grit, or quartzose gray-
wacke, weathering light-colored, embraced in the argillytes,
and interbedded with them, yet owing to upheaval and fracture
now forming all manner of contact with them, from the west
side of a point within the bay about a mile and a half west
of Stuntz island, south shore of Vermilion lake.

1965. Similar to the last, but also resembling much of the
rock on Stuntz island, from the same point, but a littie nearer
the extremity of the point.

1966. <A typical homogeneous specimen of the ‘‘ black rock,”
so-called, at the crossing of Lake street and Piedmont avenue,
Duluth.

STATE GEOLOGIST. 7

1967. A sample of the conglomerate-appearing portion of
the same black rock near the same place.

1968. Red rock, associated with this black rock near the
creek crossed by Piedmont avenue a short distance further

west.

[Note. The descriptive observations and diagrams accom-
panying these specimens, as made in the field, are reserved for
use in the final report.|

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¥ =

II.

PRELIMINARY REPORT OF FIELD WORK DUR-
ING 1893 IN NORTHEASTERN MINNESOTA,
CHIEFLY RELATING TO THE
GLACIAL DRIFT.

By WARREN UPHAM.

CONTENTS.
PAGE.
ATEAS .CXAMINE ..”. 5 5 siete che/c'< dc'a'e we lotale tthe once puebetetetere te Gale eyactey Ris ein an 19
Mapping acconrplished . 20... 00:0. 5. 5. 6 ee dam sje hlele sie elke © onion 19
TE. “"Lopography .s.é..-.<0 2's {dadaele sate Gees Se che oe ee 19
Altitudes above the sea level...) ..)s. 5... 124s seme see nee 21
BD. GeOlOGy «a: scies.b% Neti n tloake btle Ries ab steukalele: wis le cee 26
Sketch of results of Geological work. . .......).c2.'s.0.0deed esac eee 26
I. Archean outcrops in Aitkin and Cass counties.............. 26.
II. Quartzyte and Diabase in Aitkin county........... OSes 27
III. Evidence of Cretaceous beds underlying the drift........... 29
IV... Glacial drift-and moraines): +. 02.20. 2 oo c a o ee e
Transportation of boulders... 256 2.65 5 230).cs clam + eee 32
Glacial Strigw. <2 Boe ea. ask ss eka ces th eae eek eee ee 34
Deflections of giacial currents :. 2... . ves... 0s s0.s= aes eee 41
PADD sino sins ineid 6 ove bls «tale bm wipe winga'els wy cle ighajule e acalaikie bt eaten 43
Retreatal ‘moraines«..<. .. 2.02 ohn ake ealete seen ee 45
Fergus Falls moraine... 2... /t.c<. «. Teese ee 45
Leaf Hills:'moraine.. .$2..55..0. .a cee dose ae ne eee 47
TtaSCa MOraine jo). = 3. og:02 soe led ak help ee ee 49
Mesabi: moraine 2... | ck glels ole tite d son 6 a ee hee 50
Vermilion moraine 2.08.2. JS. acl eee at oe 51
Vi. Modttled Gritty. 2seei os cece oi sta ealatestc cote be wlohe Deine ene 52
Kames and ESsKers.. ..$ve.s'oi aoe cect bacite eine eieeeeiete eee 53
Valley-drift and. plains:.\5°.2o2..52). cea wed Sew ne ee ee 53
VI. The Western Superior giacial lake, and the later glacial

lakes Warren and Algonquin............... coos aie = 54

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STATE GEOLOGIST. 19

AREAS EXAMINED.

From June 6th to November 2d, the writer was engaged in
field work in the north central and northeastern portions of
Minnesota, excepting absence during the second half of Au-
gust in attendance at the sessions of the Geological Society of
America and the American Association for the Advancement
of Science, in Madison, Wis., and of the World’s Congress on
Geology, auxiliary with the Columbian Exposition, Chicago.
The areas specially assigned to me for examination and report
comprise (1) Aitkin county; (2) Cass county (excepting the
small part north of Hubbard county, assigned to Prof. J. E.
Todd); and (3) the large tract of Crow Wing county lying
northwest of the Mississippi river (which at the time of the
writing of chapter XxII in volume I of the Final Report of this
Survey, treating of Crow Wing and Morrison counties, was in-
cluded. in Cass county, being transferred thence to Crow Wing
by the state legislature in 1887).

After the examination of these areas, which occupied the
summer months, my work during September and October con-
sisted of observations of the glacial and modified drift in the
vicinity of Moose Lake, Barnum; Carlton, and Duluth; south-
westward from Duluth and West Superior to Holyoke, on the
Eastern branch of the Great Northern railway; northwestward
along the Duluth and Winnipeg railroad from Duluth to Grand
Rapids; along the Duluth and Iron Range railroad for the en-
tire extent of its main line from Duluth to Two Harbors, Tower,
and Ely, and on its Western Mesabi branch from Allen Junc-
tion to Biwabik; and along Vermilion lake, from Tower to its
outlet and western end.

‘MAPPING ACCOMPLISHED.

Having the township plats of the government surveys as the
basis for topographic (or hypsometric) and geologic mapping,
the delineations to be added were (1) lines of contour, showing
the form of the land surface in undulating or rolling tracts,
hills, valleys, and plains, with the altitudes of all portions
above the level of the ocean; and (2) the location of rock out-
crops, and the extent and boundaries of the diverse drift
' deposits.
I. TOPOGRAPHY.

For the reference of the contour lines to the sea level, the
hights determined by the surveys for the railroads of this part

20 TWENTY-SECOND ANNUAL REPORT

of the state, all of which north of Duluth and the Northern
Pacific railroad have been recently constructed, were obtained
by copying from the profiles of these surveys. Every facility
for this was courteously granted by the officers and engineers
of the several railroad companies, namely, the Duluth & Win-
nipeg, the Duluth, Missabe & Northern, and the Duluth & Iron
Range; and likewise of the shorter railroads used chiefly or
wholly for lumbering purposes, namely, the Brainerd & North-
ern Minnesota railway, the Mississippi & Northern railroad
(running northward from Cross lake, Crow Wing county), and
the Duluth, Mississippi River & Northern railroad (running

northward from Hiawatha, at the mouth of the Swan river)..

Previously I had similarly obtained and published the altitudes
determined by the Northern Pacific railroad; the St. Paul &
Duluth railroad; the Eastern railway of Minnesota (operated
by the Great Northern railway company); and hights of the
Mississippi and St. Louis rivers, and of lakes about their
sources, as shown by these various railroad lines and by sur-
veys of U. S. Engineers for the purpose of constructing reser-
voirs on the upper Mississippi and its tributaries.*

Using these altitudes, exactly ascertained by levelling, as
data for reference, careful observation and barometric readings
have sufficed for the drafting of the lines of contour, 50 feet
apart vertically, upon the areas here reported. Mainly the
surface is nearly level or only moderately undulating, but in
certain belts it rises prominently in hills 50 to 200 feet or more
in hight, consisting of marginal morainic drift accumulations
which mark the boundaries of the ice-sheet at stages of pause
or slight re-advance interrupting its general retreat at the
close of the Glacial period. The valleys of the rivers are sel-
dom very deeply eroded below the general level, their depths.
ranging from 10 or 20 feet to 100 feet or rarely more. Simi-
larly shallow or sometimes deep depressions in the general
sheet of drift hold the numerous or often very abundant lakes,
which lie commonly 10 to 40 feet below the surrounding coun:
try, and have depths of 10 to 50 or 75 feet or rarely more.

In Aitkin, Cass, and Crow Wing counties, outcrops of the
bed rocks are very rare. The thickness of the overlying
drift is believed, from its known depths in other parts of the
state, to vary from 50 or 75 feet to 150 or 200 feet, or perhaps

**A\titudes between Lake Superior and the Rocky Mountains,’’ forming Bulletin
No. 72, U. 8. Geol. Survey, 1891, pp. 229.

STATE GEOLOGIST. re

occasionally more, being spread as a somewhat uniform sheet

over that region.

The general altitude and slopes of the land

are therefore due to the form of the rock floor on which the

drift rests.

In the neighborhood of Carlton and Duluth, how-

ever, and on many large tracts of the country farther north and
northeast, the bed rocks have abundant exposures, and bold
rock hills and cliffs often show more evidently the part which
the rocky foundation takes in all the grand topographic

features.

The following table contains altitudes of the more important
railroad stations, lakes, rivers, and hills, in the region of this
report, noted in feet above mean tide sea level.

Altitudes above the Sea Level.

RAILROAD STATIONS (track).
St. Paul & Duluth Railroad.

Feet.
OUTED 7 SS Bee ae 608
BMOnt mine Park, «tive... 056: eeouoto
PITTA OMS ce ocissia, ce elas in ieee eels 1055
DSA OhIY) SAS SR a ee ana a 1083
Otter Creek station............ 1150

Summit of grade, about 1 mile
north of Mahtowa, highest on

ULI ea Wl beh (0 IS Rees eee eee eee 1170
VIDIO Walesa ioiets ate letacs,s -ieis's ofa cloves 1147
SUTTON ee ee 1105
Moose Lake station............ 1063

Great Northern Railway.
West Superior.......... Seay sis 631
Pee SUDOTION. «22.23.0500 000 672
TIS OU Hi stcrdesss < vizstevos <i cals sieve 687
RMR Ga oe oo cise .c\1 + <clas ows s BOR
PUREE a,c o/c «5 aa vo, clatne dees 956
a2 i 1025
TONY KOM Mer ces oitis\ateeniiwees ss 1100
Northern Pacific Railroad.
| OTST AE 0 peo as a 608
SOUGH SUPOTIO“ ...5...0..005.0%- 672
RAMA LSB 6c acto Ss ecie wie oc 682
1 815
OO) oS a a a 953
0 27S i 1044

Summit of grade, 14 miles south-
east of Carlton, in a rock cut

EMRE LEO UNLOR Tc sates oss tivejdisi ese « 1098
OTR Serie 2 Or a a pe 1083
Lat eR 0h: 4 eee ee 1237

Feet
OW VOTE CT he sete oe Sock ecu 1317
CTOMLWel es eh Mere we eee kk eke 1306
Wright....... Bohsbvieava is. 5 Smee 1309
PPAMIATAGK 82s wES cose tea es 1271
DECGwem OTs 5 Yancy Sek eal en's 1228
FE IMAMOTNY pap, cielo See ek ea 1237
FROSSIR Se sevact ode ee cete ates 1222
AS GIGI A. aera aet Oaa os oe Soccle ae 1208
Cedar Lake station............ 1222
ICEL WOOd te eke se eae 1277
POMESVINC he: hcaha ehmed ooicccens 1238
BAO OI 2 i a Anes oe oi Ae 1209
i B21 ELF pe rag CRU a paeneng eh Pe 1205
Gull River station... 02.60... 26 1191
Sylvan Lake station........... 1207
PARA ORES letras. aes Heeitee 1203
We elOGket ae sce era sate wih esis 1214
DIOREYS figs Fees eae cee aes 1227
U2 (EN 6 (2) ol B a ae eee etl 1255
Sta pless: Pemer Sree soe a aed! 1274

Duluth & Winnipeg Railroad.

Clequeag. tie ck ats secs otee ties 1191
TN AON AD ore. satsvae ae dn ste cows biome 1214
Stony Brook station........... 1230
Stony Brook Junction ......... 1226
GaN Se eere re teats ie sections: «ons dealers, 1237
HOOUWOOs Secs celdonsdcmeree 1255
STAN et se te he oie tesa ett cisetele 1267
Vie WALT rete Pek) hc ostape sees dav 1268
Swan River station ........... 1293
BACK DERI ih aide scissor Fy Sac es 1300
WGA TAITIGRY © citrate cee traketarte oka 1283

a shin pe
babe i pia he:
A et

22 TWENTY-SECOND ANNUAL REPORT

Feet. Feet.
SGOHASEO Ti. bl). 2c «0.» octane 1284 St. Louis River station........ 1584
Deer River station ............ 1291 . “Allen Junction Joao seer een 1508
Duluth, Missabe & Northern Railway. se ee sidin ¢ (euneesitl ; of ao
MHOPS :j, 6h. ~ soe cles es ee eee 1230 prade)).)/....: eee ites pee 1596
PIN C6 2a cc o.s\c le brett pees ta 1358 Embarras River station...... .1426
Grand Lake siding: ce. o. --.c.- 1382. Norway siding....<--..5.cccges 1472
Burnett (at the Cloquet river).1295 West Two Rivers siding....... 1426
Colum Dia... ~etieceea paisa ,.-1267. Tower Junction:..... 2. cgeaeeee 1381
ATDOrtiin 'k2.2%. cure pened ert eitertan 1301 . Tower: ..2.:2..0%.. >.> +0 See 1367
IBinCh ck arise ents erence ene antete 1320 Armstrong Lake siding........ 1475
Kelsey (at the Whiteface river)1302 Robinson Lake station..... .. 1482
AW ALTACE eielas 2 cisco crete eromtars eis wie eve. 1316 Bl ys: A eee eee 1s 3 cleric See 1417
IMOTrell eA whee cat Caries isle eters 1333 Western Mesabi Branch.
Shaw (at the St. Louis river) -.1339 Allen Junction................ 1508
AVOM IDMCMORGH: ts vo) «sus oes 2 1379 Biwabik..... sists o's wisin fa SC eee 1458
WVOl ieee techs ook nae, s's seeks 1402. MeKinley. ccs... os sscs see eae ee 1436
DM OURAN. DTOR 6 0\-nje wok «3.02 aves 1450 Virginia station (4 mile east of
Bie ete 26 ies sag nce at oe 1565 the town and about 115 feet
VAITEINIAR SSE erections cyte pistes aieloa 1439 higher) ic..:.//o,..~ 5 saeeeeeee 1555
POVGABEIIC. ai5'5 cca ae nas se Os ce 1505 LAKES.
BSW UKE rctete cole + ale!s ols creda Gitar 1455 Lake Superior, low and high

Duluth & Iron Range Railroad.

Main Line.

TOTO ET Chey 4 aH eR eR ce SARE 608
IBS HOR Matec icns hae ae eyelet tee 651
OHIO S255; isin. doo gate ree os 661
PATTY -s Stett sweet citersiortelele le eyeseets 663
AW JEL An DOLS fen tw ck cise eee ee 692
Waldo siding....... MERE nies 1057
Work. *SiGing. 23.6 55.50etaaeae 1450
Har lang is esta See eerie 1709

Summit of grade, highest on
this railroad, about 1 mile
north of Highland,in a cut of

morainic till 20 feet deep..... 1744
Whomas Siding 2. oc whose he 1610
Cloquet River station......... 1504
Breda siding: <6. s.c2 eee ae rer 1580
Bassett Lake station.......... 1636

Reno siding (summit of grade). 1676

water, 600-603; mean 1870 to

1888.6 tio. bo. on a ee 601.56
Along the International Boundary.*
South Fowl] dake:.,.:-%¢).-ceemee 1436
North Fowl lakes. o2./277. 00m 1440
Moose lake... .i..0..06. eee ee 1492
Mountain lake.../...5..2.2eepeeee 1652
Rove lakes... i002 6. cee 1667

Watershed on the boundary, be-
tween sources of the Pigeon

and Arrow rivers, about..... 1715
Rose. lakes. sc FN vee 1528
South: lake: 2 ici% cies tee ee 1558
North lakes 22: o. hs2e. ee eee 1550
Gunflint Jakes. £2. .-s3ociaeeeeee 1547
Pine: lakes sh. <5 .s60c;- oe eee 1465
Granite (or Banks’ Pine) lake. .1448
Saganaga lake..........-.---+: 1434
Swamp (or Oak) lake........... 1435

*From the profile, principally based on levelling, of the “Route by the Grand Port-
age and Pigeon River from Lake Superior to Rainy Lake,” in S. J. Dawson’s “Re-
port on the exploration of the country between Lake Superior and the Red River
settlement, and between the latter place and the Assiniboine and Saskatchawan,”’
Toronto, 1859 (pp. 45, with two maps and two profiles); corrected approximately to
accord with the recent survey of the Port Arthur, Duluth & Western railway, giv-
ing the altitude of Gunflint lake, and with the altitudes of Knife. Carp, Sucker,
and Basswood: lakes, which, as given in thisseries, besides many others south and
southeastward to the Devil’s Track lake, were determined in 1893 through levelling
by L. A. Ogaard and Alex. N. Winchell for the Geological and Natural History

Survey of Minnesota.

¥
r

STATE GEOLOGIST. 23

Feet.
Watershed between Saganaga
and Otter Track lakes,crossed
by a portage of + mile, the
only exception to a complete
circuit of lakes and streams
enclosing ‘‘Hunters’ Islaud,”

PMEMONUL De 2 orc care Asesinas Gunes. o's 1475
Otter Track (or Cypress) lake. . 1387
MERE) LICE. 5S So ereee was Sie t's’ wie) 1382
Carp (or ‘‘Pseudo-Messer’’) lake.1355
Sucker (or Birch) lake.......... 1330
PASHWOOG AKG.) 2.3... 5 woe 2c 1300
OMOOKed WAGe Lo... . 56 sens aces 1245

Lac la Croix (Nequauquon lake).1186
Crane, Sand Points, and Name-

AMMO ANCES. crs. tc. oss 2 o's ae 2 1127-1126
Rainy lake. low and high water,
PMO NCA foisee 2 <2 aleees sia a Ey

Lake of the Woods, low and
‘high water, 1057-1063; mean..1060

South of the International Boundary.t

“nT! GROSS Sas Sen ap lei
WHRCPIEUASGAP «oo occas oo oes oe 1464
Mame PeNid jl 2... 23.2506 0. tte 1355
MEP ASU TGRae aioe e diayci2) <5 02 \aisiers 1300-1302

LakeWinnebagoshish, formerly,
1290-1293; as raised by dam of
reservoir System.............. 1298

Bow String lake, head of the
Bow String river (or Big Fork

OMENAIMY TIVEL), 0.64. Soto 2: 1321
JEL SAICT SSG SE aia ate ne 1281
TELE S. 1 aE 2 ee aaa a i eee 127 55

Leech lake, formerly 1293-1295;
as raised by dam of reservoir

Pokegama lake, formerly 127];
as raised by dam of reservoir
SGI TSE GHD O ne Agee aE eAee 1275

Feet.
Sandy lake, formerly 1211; pro-
posed highest flowage by dam

of reservoir syStem........... 1220
Mille Lacs, low and high water,
1249-1254; mean............. 1251

Cross and White Fish lakes, as
raised by dam of reservoir

SVSPCUIL. aint eo a0 goer Pele eaaieadiere 1231
Maximum capacity of this dam.1236
little Boy lakes secs sade. tei 1309
Wrabado lakers = 5.0 saercnteeire 1312
Woman and Girl lakes......... 1324
er era ie Pais aie) vee aeials oie 1378
Fourteen Mile lake............ 1375
Crow Wing lake, at the head

of Crow Wing river.......... 1390
Eighth or Prairie lake, Crow

WY DITO STEM ET: cess aiaret imine beara «, tees 1385

Seventh, Sixth and Fifth lakes
of this river,respectively 1382,
1379 and 1378.

BOW laAKkG ttt ae cciciebcawew uses 1426
Long lake, Hubbard county ...1364
Slvr alee jayne hae oe severe 1201
Lower and Upper Gull lakes, as

MOWER! DYKGBIN 5 w)s-s)c o'aje/s vioeee 1200
Mee SEW DELL, dcncnat dees <6 ose 1199
Long lake, Crow Wing county

RSS ORE oe RH Ee eee 1198-1200
Pelican lake,Crow Wing county. 1211
HMbawnaSsa wes een eh -deiee 1380-1 353
Wernmlionslaker ccs. es 1357-1360
Trout lake, close north of last,

AD OMG eae at ort eset eeu fans sae 1370
Burnt-side lake, also about ....1370
Pang lake:= IBY. ie sicis'« dene ects 1337
Palisa eee at ae Gas ies cea eis 1313
INewibomlakese: Pe. wiekiemie acta ote 1307
Garden or Eve lake]............ 1384
ITP eek oe eee ees 1386
Whitewrondakens oth ..atesh 1395

+These altitudes from Red lake to Vermilion lake, inclusive. are from levelling,

mostly by railroad surveys,

but along the upper Mississippi by

United States

engineers for the system of reservoirs, aud, in the case of lake Itasca, by J. V.
Brower, Commissioner of the Itasca State Park (to whose published altitude seven
feet are here added. as required by the corrected elevation of the Great Northern

railway at Park Kapids).

*From levelling for this Survey in 1898, by L. A, Ogaard and U. 8S. Grant. The

altitudes of Trout and Burnt-side lakes, and of others

following, when not

specially indicated, are from barometric readings by Prof. N. H. Winchell, Dr. U.S.
Grant and Mr. A. H. Elftman, referred to sea level approximately by comparison

with the hights ascertained by levelling.

+From surveys for extension of the Duluth & Iron Range railroad.

24 TWENTY-SECOND ANNUAL REPORT

Feet Feet.
Birch-lakes. i... ss 2s bw teen ee 1410 Mouth of Sandy river, low and
Slate lake (T. 60, R. 10)........ 1640 high water. :¢.. cba. ae 1210-1224.
Greenwood lake (T. 58. R. 10)..1705 At Aitkin, low and high water
Seven Beaver lake............. 1 Cy GYR ee ER A 1190-1200
Gabbro Jake . ©. 2.0 aes nee 1464 Mouth of Pine river, ordinary
Bald Magilejlake: ?2.2.08), sje. - 1468 low stage: ... .: ashen 1177
Bake Isabelle :.2 aces ee ee ne 1570 At Rice lake, two miles north-
Snowbank lakej.s. os = smess.-\2 «ts 1424 east of Brainerd,held by dam.1172
Wilder‘lake) :..sv< sen tee caer 1540 At Brainerd, low and high
make AlICe..\:.5— peek aes b ac 1544 Waters. .tic..2.) hoe eee 1150-1167
"Thomas lake.i\ 50 Ao secon ee 1534 Mouth of Crow Wing river, low
Fraser lake..... rte Sale We ato lee 1535 and high water.......... 1145-1163
Kekequabic lake*........ ey ae 1497 At Little Falls, above and be-
Syenite lake (T. 62, R. 6 W.)...1777 low the dam >... 24 sue 1099-1079
Lake Polly (T. 63, R. 6 W.)....1617 At St. Cloud, above and below
Little Saganaga lake* ......... 1600 the daii.2 f.. 22s: eee ee 975-960
Gabemichigama lake* ......... 1587 At Minneapolis, above and be-
Ogishke Muncie lake*......... 1488 low St. Anthony’s falls....794-738
pea Gall lAKe ween sonic alee ese 1440 AtSt. Paul, lowand high water
West Sea Gull lake ............ 1455... sb. sa ee bee 683-702
Gake Ida-Belle®... 00.2 6 uses 1793
Kiskadinna lake*.............. 1767. Crow Wing river and its tributaries.
Mayhew and Iron lakes*....... 1853 Note.—The hights of Crow Wing
GOON AK Stor 08s soho wiontele setaios 1745 and lower lakes, forming a series
PSTUE, Valeen att se at ei caststais’ 2 see es 1851 on the ‘head stream of the Crow
Wirchell*lake*..<2 8 12h eiseneete 1910 Wing river, are given on page 93.
Gaskanas 1aice” sn 2c\jeeeeinee'e 1878 The survey of the Great North-
Meals Talkies... iss s)s.oes ioe eejenyee 1879 ern railway branch to Park Rapids

Lake Abita, probably the high-

est in the state, on the south-

ern slope of Brulé mountain*.2048
Devils Track lake*.e3.2.<% Jens 1636

RIVERS.
Mississippi river. :
Novre.—See lakes Itasca, Pemidiji,
Cass, and Winnebagoshish, in the
preceding list.
Head and foot of Pokegama
falls, as raised by dam. .1275-1254
Head and foot of Grand rapids,

qmilelonge. ts. 2550 2's 1253-1248
Mouth of Split Hand river..... 1236

Mouth of Swan river........... 1226

supplies the following altitudes of
tributaries of the Crow Wing river
at the bridges of this railway:

heat riverer..- eee pie “eh, 1293
Blueberry, river-.<.1... a0 2) wee 1372
Shell -river.<.5.\.4.. see eee 1379
Straight river:.'. 13> sade ements 1402
Wish-hook Tiver.?.<.cee. seer 1424

Crow Wing river at Motley....1208

Junction of Crow Wing river
with the Mississippi. low and
high water... .. 25. oseer 1145-1163

St. Louis river and its tributaries.

Embarras river at bridge of the
D. & I. BR. railroad......-.. . 1410

*From levelling for this Survey in 1893, by L. A. Ogaard and U. S. Grant.
The altitudes of Trout and Burnt-side lakes, and of others following, when not
specially indicated, are from barometric readings by Prof. N. H. Winchell, Dr. U.S.
Grant and Mr. A. H. Elftman. referred to sea level approximately by comparison

with the hights ascertained by levelling.

+From surveys for extension of the Duluth & Iron Range railroad.

STATE GEOLOGIST. 25

Feet.
Lakes of this river, extending
in a series about 12 miles,
where it passes through the
Giant’s (or Mesabi) range and

BOUUMWATA. 5 \..2 5c jalewies 1380-1353
Cloquet river at bridge of the
Peo. BR. railr6ath.......2..-.- 1479

Small lakes forming the head
of the St. Louis river, in the
west part of T. 59, R. 11 W.,

TDR EAE AA oc, SEUAe ey Seen eae 1685
Expansion of this river in Seven
OAV GTS AKGE Sc eats lec ee ec sis cs 1675
St. Louis river at bridge of the
Waco. TATTOAG, ..- .. <6 1584
At bridge of the D., M. & N.
2) a eres 1300
At mouth of Floodwood and
Hast Savanna rivers...... ..-1234
At Stony Brook Junction...... 1211
At Cloquet, head of rapids above
POTN ECR ANN «oe seco ve cic sis «anid te 1178
Poonor Knife falls: onc. 6... . 1160
At bridge of the D. & W. rail-
POM Soe cei ois Sait wate. shi 1120

‘Top of dam at Thomson, about. 1040

At bridge of the St. P. & D. rail-
road, close below the last, low
and high water.......... 997-1020

At Fond du Lac, level with lake
Superior, about seven miles
easinOt LHOMISON® -).). 5: 4015.25. 602

HILLS AND MOUNTAINS.

Highest point on the road from
Brainerd to Leech lake, about
seven miles south of the In-
dian Agency........ atctopcee 1500

Summit of ridge southwest of
Pokegama lake, in the south
part of T. 54. R. 26, the high-
est point in Itasca county... .1617

Poquodenaw mountain, sec. 25,

T. 52, R. 26, the highest hill
in Aitkin county, about...... 1525

Feet.
Hills in secs. 26 and 28, T. 59, R.
17, about four miles northeast
and three miles N. N. #. from
Virginia, forming the highest
land in St. Louis county, re-

spectively, about....2025 and 2150
Summits of the Giant’s (or
Mesabi) range, in T. 59, R.
16, a few miles north of

Biwrapiice ns). A eae 1800-1900
Summits of this range near
Hinsdale, where it is crossed,
in a gap, by the D. & LR.

ATOR ears a aie oe oe 1850-1950
Hill close north of ‘Tower
(South ridge}, about.......... 1560

Soudan hill (North ridge), one
mile northeast from the last,

UI OMS we. nte nso che eo oe tae er octetete 1600
Jasper peak, 24 miles east of
ROWE CUOUbet s O22 Sep 6 s ta,3 1650

Ridge close southeast of Syenite
lake, in the east part of T. 62,
R. 6 W., probably the highest
in Lake county, about. .2100-2200
Misquah hills, Cook county, the -
highest in Minnesota, in the
south edge of Ts. 64, Rs. 1
and 2 W., comprising several
summits about 2200 feet above
the sea along a distance of
eight miles from east to west,
with their highest point
about a half mile southeast
from the eastend of Winchell
lake, determined by levelling.2230
Brulé mountain (T. 63, R. 1,
Wiaby levelling? s 25.2 <5’. 2170
Top of bluffs (600 to 700 feet
above lake Superior) close
north of Duluth........ 1200-1300
Sawteeth mountains, near the
shore of lake Superior, from
Temperance river and Carl-
ton’s peak to Grand Marais
Berna aeisieye mites. «nF Matin > LeOO-1700

26 TWENTY-SECOND ANNUAL REPORT

II, GEOLOGY.

In the areas assigned to me for geologic mapping and re-
port, namely, Aitkin and Cass counties, and the northwestern
part of Crow Wing county, the tracts covered by the several
varieties of the glacial and modified drift have been delineated
approximately. The few and small outcrops of the bed-rocks
have also been shown on the maps; but, in a region so almost
universally drift-covered, it is impossible to trace with cer-
tainty, or perhaps even with demonstrable probability, the
limits of these Archean and Taconic formations. Under many
portions of the drift-sheet here Cretaceous beds, though not
observed in outcrops, are doubtless still thinly represented in
place. Onamap of the formations underlying the drift, the
northwestern part of Cass county is best shown as Cretaceous,

and this may also extend eastward through Aitkin county; for —

itis known that much of the drift of these counties has been
derived from contiguous and underlying Cretaceous shales by
glacial erosion.

SKETCH OF RESULTS OF GEOLOGICAL WORK.
I. ARCHEAN OUTCROPS IN AITKIN AND CASS COUNTIES.

A considerable tract in the southeastern part of Aitkin
county is probably occupied by Archean rocks, which extend
thence east and south into Pine and Kanabec counties. Be-
tween the Snake river and Cowan’s brook, in the south edge of
Aitkin county, the glacial drift in the S. E. 4 of sec. 34, T. 48,
R. 28, has in some places very plentiful blocks of a fine-
grained, gray granite, containg black mica. This Archean
formation is doubtless the bed-rock there at a little depth be-
low the surface. Within a mile southwestward, and thence for
nearly three miles down the Snake river, past its Upper and
Lower falls in northern Kanabec county, Archean granites,
schists, and gneiss, have many and extensive outcrops.

In the most southwestern township (T. 134, R. 32) of Cass
county, the east half of sec. 28, about five miles northwest from
Motley, comprises an area of frequently outcropping horn-
blendic granite, extending a half mile from south to north,
with a width of twenty to forty rods. These rock exposures
rise five to eight feet above the adjoining general surface of
moderately undulating drift, being twenty to forty feet above
the Crow Wing river, which lies about three-fourths of a mile
to the southwest. Two wide dikes of dark, tough diabase in-

STATE GEOLOGIST. 27

tersect the granite, following the course of nearly vertical
joint planes. In the Eleventh Annual Report (pages 87, 88),
these rocks are described in detail, and a figure is given show-
ing a part of one of the dikes, with narrow branches running
from it. Some portions of this granite may be found valuable
for quarrying, which, though several times contemplated, has
not yet been undertaken.

Il. QUARTZYTE AND DIABASE IN AITKIN COUNTY.

Quartzyte forms a slightly projecting point of the north-
western shore of Dam lake, near the center of the west half of
sec. 35, Kimberly (T. 47, R. 25), about three miles south from
Kimberly station and eleven miles east of Aitkin. Its outcrop
has a length of about 250 feet along the shore and varies in
width from 15 to 50 or 60 feet, rising to a hight of four or five
feet above the lake. Through all its extent the rock is much
fractured into separate boulder-like masses from one or two
feet up to ten or rarely twelve feet in diameter, lying in close
contact, with only very scanty foreign drift boulders of gran-
itic, trappean, and other crystalline rocks such as abound in
the drift of all this district, and even in the immediate vicinity
of the outcrop. Boulders of the quartzyte, however, are very
rare in the drift, and the great abundance of its masses at this
_ locality shows unquestionably that it is here the bed-rock,
although no compact ledge is seen. The shattered condition
of its whole observable extent seems probably attributable to
preglacial weathering of the rock at and near this place to
form low cliffs with many boulders due to gradual disintegra-
tion along crevices and joint planes. During the Glacial
period some or perhaps all of these quartzyte masses may
have been transported short distances, but the very small pro:
portion of boulders of other rocks mingled with the quartzyte
indicates that its blocks are in or near their preglacial position.

In its original condition this rock was a sandstone of well-
rounded white quartz grains mostly from a thirtieth to a
tenth of an inch in diameter. The spaces between the grains
have become filled with similar white quartz, and the rock is
now a very compact light gray quartzyte, varying rarely in
superficial portions to a partially reddish color where iron per-
oxide coats the sand grains and stains the interstitial quartz.

Apparently the most probable hypothesis that we can
assume, in attempting to correlate this Aitkin county quartzyte
with the stratigraphic sequence of rock formations ascertained

28 TWENTY-SECOND ANNUAL REPORT

elsewhere in all the surrounding country, is to suppose it to be
apart of some area, very probably a belt having a general
east-northeast to west-southwest extension, of the Pewabic
formation, which is regarded as the basal member of the
Taconic series. There may be, according to this hypothesis, a
wide and shallow synclinal trough of the quartzyte with its
northern border on the southern slope of the Giant’s (or
Mesabi) range, with western continuation to Pokegama falls
on the Mississippi, and its southern rim represented by the
locality here described. The dip and strike of the strata,
however. were not determinable in this place, since no distinct
lines of bedding were observed in any of these quartzyte
masses; and their irregular forms, although evidently due to
joint structure, indicate that the formation here is not trav-
ersed by any regular systems of parallel and intersecting
joints.

About three miles southwest from this exposure of quartzyte,
two outcrops of nearly black, rather coarse-grained, very hard
and tough diabase occur in the S. W. 4 of sec. 9, T. 46, R. 25,
within about a fourth of a mile west from the south end of
Long lake and some 20 or 25 feet above it. A foot trail leading
from Rabbit lake northeasterly to Dam lake passes over the
western and larger outcrop, which has a smooth and somewhat
flat extent of about 100 feet from southwest to northeast, with
a maximum width of 30 feet, rising only one to two feet above
the general surface of the glacial drift. This trap rock shows
no traces of flow or shear structure, nor any noteworthy varia-
tion in the degree of coarseness of its crystalline texture,
throughout its visible area. It belongs doubtless to the central
portion of a dike of undetermined but probably not very great
width, whose borders and contact with the country rock on
each side, presumably quartzyte, are hidden by the drift.

The course of the dike is probably from southwest to north-
east, for a second exposure of the same rock is found at a dis-
tance of about twenty rods farther northeast, divided from the
foregoing by a slight depression of five feet in which there is
a grove of several large poplars. The length of this outcrop
is about 30 feet, also trending northeastward, and its width 15
feet. Both outcrops are cut in many directions by numerous
joints, nearly vertical or steeply inclined, among which no
prevailing system is observable. Slight weathering of these
rock surfaces has removed their glacial striation;but the diabase
appears to have been more durable to resist decay than the

STATE GEOLOGIST. 29

enclosing strata of the country rock, for which reason the dike
remains with a greater hight and projects through the drift
sheet. A wooded hill of the drift rises within a distance of
about a quarter of a mile northeastward toa hight of 40 feet
or more above the trap outcrops, which lie in a tract having
only bushes and scattering small trees. An examination for a
considerable distance around failed to discover other rock ex-
posures, but very probably some of small extent will be found
if the land should be cleared for cultivation or pasturage.

The time of the volcanic or more deeply seated plutonic in-
trusion of the trap rock here cannot be definitely stated. Quite
probably it may have been contemporaneous with the intrusive
laccolitic sills of diabase in the Animikie and Keweenawan (or
Nipigon) sedimentary formations on the northwest coast of
Lake Superior. Dr. A. C. Lawson concludes that those trap
sheets and dikes, mostly similar to the diabase in Aitkin
county, are of some undetermined age subsequent to the Ke-
weenawan period, which was in the later part of the Taconic or
Algonkian era.* They may belong, however, to a very late
stage of this era, before’its great upper series of detrital and
volcanic rocks was completed.

Ill. EVIDENCE OF CRETACEOUS BEDS UNDERLYING THE DRIFT.

Although no outcrops or natural exposures of Cretaceous
strata have been found in Aitkin and Cass counties, it seems
highly probable that shales of this age remain in many places,
perhaps upon the greater part of this area, beneath the drift.
Fifteen years ago Prof. N. H. Winchell wrote:

A line drawn from the west end of Hunters’ Island, on the Canadian
boundary line, southward to Minneapolis, and thence southeastwardly
through Rochester to the Iowa state line, would, in general, separate
that part of the state in which the Cretaceous is not known to exist from
that in which it does. It is not here intended to convey the idea that
the whole state west of this line is spread over with the Cretaceous, be-
cause there are many places where the drift lies directly on the Silurian
or earlier rocks; but throughout this part of the state the Cretaceous
exists at least in patches, and perhaps once existed cuntinuous?y.T

This opinion has been well confirmed by the subsequent
work of this Survey, and notably by Mr. H. V. Winchell’s
recent discoveries of Cretaceous shales at several places 35 to
45 miles northeast of Aitkin county, along the elevated Mesabi
range.{ The Cretaceous marine submergence of this region

*Bulletin No. 8, of this Survey.

+Bulletin of the Minnesota Academy of Natural Sciences. vol. i, p. 348.
tAm. Geologist, vol. xii, pp. 22-223, Oct., 1893.

30 TWENTY-SECOND ANNUAL REPORT

appears thus to have extended eastward at least to the present
site of lake Superior. A large part of the clay of the glacial
drift here was doubtless derived by erosion from Cretaceous
shales, and their calcareous matter supplied to the drift may
principally account for its small amount held in solution by
wells and springs in these counties, making their water some-
what ‘‘hard” and unfit for washing with soap.

On the site of the Sandy lake dam an excavation about ten
feet square, made in the summer of 1893, encountered in the
modified drift, ata level a few feet below the river bed, a
gravel layer enclosing abundant water-worn and partially
rounded lumps of lignite. These masses vary in size from
one or two inches to six inches or more in length, and are
mostly flattened in parallelism with their bedding planes. It
was estimated by Mr. Archibald Johnson, in charge of the
construction of the dam, that about two bushels of lignite
fragments were thrown out from this small excavation. They
are of quality similar to the lignite coal found in thin layers
enclosed in Cretaceous shales near Richmond, Ft. Ridgely,
and Redwood Falls in Minnesota, and to the thicker Cretaceous
lignite beds which are mined on the Souris or Mouse river and
west of Bismarck in North Dakota. Small fragments of
lignite are found very rarely in the till of all the western two-
thirds of Minnesota, including Aitkin county, in which Sandy
lake is situated; and gravel layers in wells near Aitkin occa-
sionally contain smoothly rounded pebbles of. very compact,
nearly black, carbonaceous shale, somewhat resembling graph-
ite. Occurring so plentifully at Sandy lake, this lignite
gravel must have been derived from the erosion of some layer
of lignite in’ Cretaceous shales not far distant northward or
northeastward.

Only very scanty Cretaceous shale gravel, however, is found
in the till and in nearly all the modified drift of this region.
The greater part of the Cretaceous beds here may be too soft
to yield pebbles, the product of their glacial erosion being
principally an indistinguishable part of the fine rock flour or
clay in the till. The lignite fragments at Sandy lake are not
sufficient, according to the opinion of the writer, to indicate
the existence of workable layers of lignite; for they more prob-
ably came from thin seams like those known elsewhere in Min-
nesota, which are mostly about one foot or less in thickness
and nowhere exceed three or four feet, being inadequate for
profitable mining. Little or no encouragement can be given

STATE GEOLOGIST. 31

to prospecting in this thickly drift-covered region with the
hope of finding valuable beds of this brown coal.

IV. GLACIAL DRIFT AND MORAINES.
(Mapped in Plate I, facing page 18, at the begining of this chapter.)

Nearly all of Minnesota is covered by a mantle of drift that
averages from 100 to 150 feet in thickness, almost everywhere
concealing the bed-rocks, which generally had been subaérially
eroded in preglacial times to an approximately flat or only
- moderately hilly surface. Small knobs and hills of rock which
had been spared by the preglacial erosion were doubtless in
many places worn down and levelled by the ice-sheet, and its
drift was filled into the preglacial valleys, so that the contour
of the drift-enveloped country is now more uniform than it was
before the Ice age. But on certain belts the drift was left in hills
and ridges, accumulated along the margin of the ice where it
paused or somewhat reiidvanced, apparently because of secular
fluctuations of climatic conditions, at successive stages which
interrupted its general retreat during the closing part of the
Glacial period. Numerous belts extending across areas which
have a nearly plane surface of the underlying rocks are thus
occupied by drift amassed in prominent hills. Upon the greater
part of Minnesota the only hills are formed of this morainic
drift, ranging in hight commonly from 25 to 75 or 100 feet, but
occasionally attaining much greater altitude, as in the Leaf
hills, which rise from 100 to 350 feet above the moderately
undulating country on each side. These characters of the
bed-rock contour, and of the overlying drift surface, prevail
through Cass, Crow Wing, and Aitkin counties, and the region
thence north to the international boundary, as also upon most
of the area eastward to the sources of the St. Louis, Whiteface,
and Cloquet rivers.

Farther northeastward, a region of comparatively scanty
drift, with plentiful rock outcrops, begins upon Rainy lake,
Net, Pelican, and Vermilion lakes, in the Giant’s or Mesabi
range (a high granite ridge), and along the bold highland
which forms all the northwestern shore of lake Superior. This
region, reaching thence northward and eastward into Canada,
presents very remarkable contrasts with the other and far
greater portion of Minnesota before described; for it has fre-
quent steep rock hills 100 to 200 or 300 feet above the neigh-
boring lakes and streams, and its drift averages probably only
from 10 feet or less to 25 or 50 feet in thickness, often giving,

SO a

32 TWENTY-SECOND ANNUAL REPORT

even on the lowlands, ample opportunities for examination of
the older geologic formations, and for accurate tracing of their
boundaries. Yet this hilly and rocky district is quite surely
less uneven than before its glaciation, which in general tended
to reduce the hights of the hills and to fill the hollows with
drift, or to bar them with drift accumulations whereby most of
the very abundant lakes of the district are partially enclosed.
In many instances it may be shown here that glacial erosion
produced rock basins that are filled by lakes; but more com-
monly some part of the lake shores consists of drift whose
removal would open avenues through which the water could
mostly or wholly flow away.

Transportation of Boulders.

The boulders of the drift in northeastern Minnesota have been
mostly transported toward the west, southwest, and south, from
their parent ledges. In the northwestern part of the state,
however, the glacial currents flowed and carried their boulders
from the Silurian limestone region of lakes Winnipeg and Man-
itoba, and from the Archean gneiss and granitic rocks east and
north of lake Winnipeg, southward and southeastward into
western and southern Minnesota, and thence continued across
Iowa to the drift boundary in Missouri and northeastern Kansas.

These two fanlike outflows from the farther north and thicker _

central portions of the ice-sheet were confluent, pushing
against and uniting with each other from the northeast and
northwest, along a belt which extends southward from near
the mouth of Rainy lake and Winnebagoshish and Leech lakes
to the vicinity of Brainerd and to Minneapolis, coinciding ap-
proximately, for this distance of about 250 miles, with the
courses of the Big Fork (or Bow String) and Mississippi rivers.

Throughout the district of this field work and report the
drift is mainly derived from the rock formations outcropping
and underlying it within distances from a few miles up to fifty
miles in the directions whence the glacial outflow advanced.
Upon an area of gabbro, or of granite or schists, or slate, or
other rock, and for some miles onward, many of the boulders,
large and small, and much of the gravel in the till and modified

drift, consist of the same kind of rock. The glacially eroded —

grist comprises frequent boulders up to 5 feet in diameter,
usually very few up to 10 feet, and exceedingly rare biocks of
larger size, excepting near to prominent and favorably jointed
rock outcrops, A much larger proportion of the drift occurs

STATE GEOLOGIST. 33

as small boulders and fragments, gravel, sand, and rock flour,
the fine detritus making nearly everywhere the far greater
part of the whole mass.

Only where rock formations of restricted area have peculiar
characters by which their boulders can be identified with cer-
tainty, as distinct from all similar boulders supplied by other
formations and districts, is it possible to affirm positively the
distance of their transportation. Thus, we find rarely in Big
Stone and Otter Tail counties, of western Minnesota, granite
*poulders with included fragments of hornblende scnist,* like
much of the granite forming the Giant’s or Mesabi range, which
was probably their source. These boulders appear to have
been carried about 200 miles southwest and west-southwest. A
mass of native copper weighing more than thirty pounds, found
in Lucas county, southern lowa,+ had been doubtless borne by
the currents of the ice-sheet about 600 miles, from the present
copper mining region south of lake Superior, or from Isle Roy-
ale, first southwestward and then southward through eastern
and southern Minnesota, passing west of the Wisconsin drift-
less area.

The farthest known transportation of rock-fragments in the
drift, recorded in part by Dr. Robert Bell, of the Canadian Geo-
logical Survey, whose observations are supplemented by my
own, is from James bay southwest to North Dakota aud Minne-
sota. The rock thus recognized is a ‘‘dark grey, granular,
siliceous felsite or greywacke,...... characterized by round
spots, from the size of a pea to that of a cricket ball or larger,
of a lighter color than the rest of the rock, which weather out
into pits of the same form.” It occurs in situ, as reported by

_Dr. Bell, on Long island, off Cape Jones, on the east coast of
Hudson bay, where it is narrowed to form James bay, having
there a southwestward strike, and probably continuing under
the sea for some distance in that direction. He notes that the
abundance of pebbles and boulders of this rock is the most re-
markable feature of the drift on the west coast of James bay
and along the Attawapishkat, Albany and Kenogami rivers,
and that its fragments have been found by him as far west as
Lonely lake, and southward to lake Superior.{ Farther to the
southwest and south I have observed fragments of it, usually

* Final Report, vol. i, p. 626; vol. ii, p. 551.

+C. A. White, Geology of Iowa, 1870, vol. i, p. 96.

+ Geol. and Nat. Hist. Survey of Canada, Annual Report, new series, vol. ii, for 1886,
p. 36G; compare Report of Progress for 1878-79, pp. 22, 230.
—3

34 TWENTY-SECOND ANNUAL REPORT

only a few inches, but in some instances, a foot or more in
diameter, occurring very rarely in the drift in the northeastern
part of North Dakota, where the largest piece ever found by
me was about thirty miles south of the international boundary
and fifty miles west of the Red river, and at numerous localities
in Minnesota, where it extends at least as far south as Steele ©
county, seventy five miles south of St. Paul, and a thousand
miles southwest of its outcrop north of James bay.

GLACIAL STRLE. | :

While the most distantly derived boulders of the drift bear
testimony of the sum of all the movements of the glacial cur-
rents, during the entire Ice age, upon the area across which they
came, itis to be remarked that the glacial strie, or furrows
and scratches on the bed rocks engraved by boulders, pebbles,
and sand grains frozen in the base of the moving ice-sheet
record only the course of the latest glacial current there, ex-
cepting such striated rock surfaces as became drift-covered
and thus protected from the latest ice abrasion. Probably the
average glacial erosion of our. rock surface, for different parts
of Minnesota, varies from 10 or 20 feet to 50 or 100 feet or more,
approaching, but not generally equalling, the depth of the
drift. Nearly all of the strize produced during the early and
middle portions of the Glacial period have therefore been
erased and their places taken by the later markings. Even
where one set of strize was protected by a drift covering until
a considerably divergent set was engraved on adjacent parts.
of the same ledge, as has been observed at some localities in
southwestern Minnesota,* and in many places near Duluth,
noted in the following table, it is far more probable that both
belong to successive late stages of the glaciation than that any
long fraction of the Ice age intervened. When several courses.
intersect each other on the same rock surface, differing 30°,
60°, or even 90°, in their extremes of defiection, as in numerous.
instances near Carlton, Thomson and Duluth, these varia
tions seem referable to the closing scene of the glacial re-
treat when the ice border, irregularly indented in its process
of melting and consequently having sudden and great deflec-
tions of its marginal currents, was being withdrawn across.
these striated rock exposures.

Generally outcrops that have been long exposed to the disin-

*Pinal Report, vol. i, pp. 505.and 549, with figures 35 and 44.

STATE GEOLOGIST. 35

tegrating action of the weather, having been undoubtedly in
many instances bare ever since the departure of the ice-sheet,
show few remnants, or only here and there faint traces, of
their originally abundant striz. These long weathered rock
surfaces have suffered a slight loss, estimated to vary com-
monly from a sixteenth of an inch or less to a half inch or
sometimes more, worn away,with the delicate glacial striz, by
the rains of many centuries, while yet the planed or rounded
forms of the ledges due to their glaciation are unchanged.
That so little subaérial erosion has taken place since the end of
the Ice age is a sure evidence of the geological brevity of this
Postglacial or Recent period, agreeing with the conclusion
reached by Prof. N. H. Winchell from his investigations con-
cerning the rate of recession of the Falls of St. Anthony, by
which he estimated the length of postglacial time to be about
8,000 years. t

Wherever the ledges have been covered by drift and so pro-
tected from weathering, they retain their glacial marks in per-
fection; and on tracts of plentiful rock outcrops, such striated
surfaces are frequently exposed by excavations for streets, cel-
lars, etc., and by the removal of the drift on the borders of
quarries. Though most of the striz of naturally exposed
ledges have become effaced, usually a careful search will de-
tect some portions where they remain; and occasionally, even
on surfaces evidently exposed during all the Postglacial period,
the striation is still very distinct upon spaces 10 to 20 feet or
more in extent.

Courses of Glacial Strie in northeastern Minnesota,
referred to the true or astronomic meridian.

FROM NOTES BY COL. CHARLES ales ees TaKGy, Sag sire: ep Bs ea se

x ITO M Aes 5 ephi.3 sae gee . 48° W.

Pa eee: Island in Carp lake....... S. 40° W

Mermilton lake.......-...- SE Led AWN sige = LAGGED DANCES 25 aces ciate, sje%eid aw a: fiei ce 2 S. W.
Sand Points lake.......... S. 55° W. Basswood lake, Northeast cape

Namekan lake. also..... See smn Ewe bP cee. aoe ee 8 caus 5. 15° W.
Rainy lake....... S. W. toS. 75° W. Ima lake, north shore..........

Big fork of Rainy river at ‘a
fall of six feet over trappose
rock,” estimated 82 miles by
the stream from its mouth
0 1 N. 80° W.

FROM NOTES BY ProFr. N. H.
WINCHELL, in former annual re-
ports of this survey.

gelesen S. 36° W. and S. 23° W.
Island in Thomas lake....S. 25° W.
Seca ll, i G4 cow. os. ct. S. 30° W.
Delta lake, sec. 28, 'T. 65, R. 6.

ek oh, CaM Oe = aA Se Si 250 W.
SEC OO MOSES Ole ws: sare cals S. 8° EB:
Sec. 35, T. 63, R. 9 eh ae S. 12° W.
Sec. 27, fhe 63, OM nectele S. 15° W.

Birch lake. .S. 12 °W. and S. 22° W.

+Final Report, vol. ii, pp. 314-341, with maps and plates,
* Report of Explorations in the Mineral Regions of Minnesota during the years

1848, 1859, and 1864.

36 TWENTY-SECOND ANNUAL REPORT

Vermilion lake, twenty locali-
MICS ces tiny o> aa eee S. 17°-24° W.,
and three other localities ....
eesiee S. 28° W., S. 10° W. and S.

Pike river, tributary to Vermil-
ion lake, two places..........
ee PE eae S310°. and.20° W.

Dialuth:.. 5.) aces eee W.S. W.

Prairie river, lower falls, sec. 34,

T. 56, R. 25 W S. 10° E.

FROM NOTES BY MR. HORACE V.
WINCHELL, in the Sixteenth and
Seventeenth Annual Reports of this
Survey.

Little fork of Rainy Fes five

localities 2. <jse.0 teens S. 10°-42° W.
Rainy river, 34 miles below Ft.

WranGis: 2427; 46s. 085 S. 32° W.
Rainy lake, nine localities......

Dees ati aras cote oe S. 32°-64° W.
North fall on outlet from Name-

kan lake to Rainy lake. .S. 30° W.
Bow String river (Big fork of

Rainy river), probably in T.

63, R. 26, intersecting strie.

mainly.....S. 10° W. and S. 30° E.
dG:,i* short distance above

the last, very distinct glacia-

CiGAS ©: 8. chins eee sor atee S. 60°

[or, more probably ....N. 60° W. ]
Deer river, at dam about a half

mile above its junction with

the Big fork, probably ine ee:

62, R. 25. .S. 80° E. to due E.

cafe nite oats or, N. 80° W. to due W. ]
Big fork, about three miles

above ‘the mouth of Deer
Due E.

cae nad for more probably, W.]
do., in or near sec. 36, T. 150,

R. 25......8. 52° E. for N | 52° W.]

The cause of the foregoing Te-
markable deflections will be con-
sidered on a following page.

Net lake, in the Bois Fort In-

dian Reservation... .S. 20°-24° W.
Pelican lake, mostly in Ts. 64

and 65, R. 20, four localities

hs rey Pod ee S. 24°-36° W.
Elbow lake, T. 64, R. 18, two

localities. .S. 26° W. and S. 28° W.
Trout lake, north of Vermilion

lake, two loralities...... ....

5 ae 8. Ae S. 16° W. and S. 36° W.
Summit of the Giant’s range at

Hinsdale $25 tiie. wean ob S.222 W.
Sec. 32, T. 60, R. 13, about..S. S. W.
Sec. 35, T. 61, R. 12, south of

Birch lake, about...S. 12°-30° W.
Sec. 10, T. 64, R. 8, south gee

sign lake:.. Seca. S. 24° W.

Sec. 27, T. 64, R. 8, northeast
end of Disappointment lake..
er ete S. 34° W.

Sec. 36, T. 62, R. 8, south of lake
Isabelle-¢.- seeceemeess S. 24° We

Sec. 15, T. 59, R. 6, southwest of
Crooked lakes; sis acaeee S760 We

FROM NOTES BY Dr. U. S. GRANT,
1892-93.

N. W. tof sec. 27, T. 65, R. 2 W.,
north shore of lake Louise..
piss elo eoincs sae see S. 16° W.

S. E. 4 of sec. 28, "T..'65, ees
W., north shore ‘of lake Emma
igeae decals «aid SC a:

N.. W.-2 of sec. 35, FT. 65,5
W., north shore of No-name

Jakes pote 4s>.. 3.32 Pee S.. 2°oWe
S. W. 4, sec. 10, T. 63, R. 3 W.,
reef in Brulé lake....... S. 18° W.

S. E. 4, sec. 20. T. 65, R. 4, north

shore of a small lake.. ...S. 4° E.
N. W. i, sec. 13.'T. 64, R. 6.8. 28° W.
N. E. , sec. s Ss Bae R. 6, on an

island*..; = 2.222 S. 50° W.
N. E. 2, sec. 7, T. 65, R. 6, island
in Amceba lake 3s eee S=30? Wi

S. W. 4, sec. 35, T. 66, R. 6, north

end of island in lake Avis.S. 30°W. —

FROM NOTES BY PROF. G. E. Om
VER, 1893.

Pokegama falls, Mississippi
river [201.4462 S. 50°
Prairie river,lower falls. 8. 4°-10° E.

On tne Bow String river(Big fork
of Rainy river):

First rock outcrop observed in
descending this stream...S. 5° E.,
and nearly due E. [more prob-
ably W.]

“Another exposure of diorite
some five miles down the
stream”...S. 70° E. [or N. 70° W.]

Foot of Rice River rapids, on
the “upper exposure of green-
STONE? 5c. ais\s eee ae S. 35° E.;
and on its ra exposure. .
nil o5 aes poets S. 65° E. [or N. 65° W.]

A few miles below the last...

...-9. 10°-80° E. [or N. 70°-80° W.)

A short distance farther down
the river S. 70° E. for N. 70° W.]

About. halfway between the
mouths of Rice and Deer rivers

_..S. 70°-80° E. [or N. 70°-80° W.]

An eighth of a mile above es
Aaittletalls.....52: $s. 2 52 seme S.2°E.

Little falls..... 22a S. 2°-8° E.

STATE GEOLOGIST. 37

Rock gorge of river, + mile long,
estimated 12 miles below the
Mimnpleyealise...% 2.0.08 ces mesos
....8. 58°-70° E. [or N. 58°-70° W. |

Big falls.....S. 80° E. [or N. 80° W.]

14 miles below the mouth of
Sturgeon river (which comes
in from the west 5 miles be-
low the Big falls) ....... S. 24° Bi.

About 12 miles below the Big
falls.S. 58°-62° E. [or N. 58°-62° W.]

About 25 miles below the Big
falls,on the lowest rock out-
crop observed on the Big

PEIN. Ye User as oe S. 44° W.

Little fork of Rainy river, 4
miles from its mouth...S. 50° W.

Rainy river, 2? miles below Ft.
WUT Me eee shone SS isis S. 40° W.

do., 14 miles below Ft. Francis.
PAGER Rees cco G abee: oie S. 40° W.

Near the head of Black bay of
ety lake... < o.:- 2... S. 52° W;

Westend of Namekanlake.S.40° W.

Sand Points lake.10 miles from
the mouth of the Vermilion
MMOVIESTGRCS Sev sisye tte chore cists v.06 S) 220 We

FROM NOTES BY MR. W. H. C.

SMITH.*

Near Sand Points lake....S. 28 °W.

Knife and Carp lakes. .S. 10°-38° W.,
averaging about........ S. 23° W.

Otter Track (Cypress) lake and
Cache bay at west end of Sag-

anatanake.........9- 10°-28° W.5.

most commonly about..S. 20° W.
Extreme limits of all the ob-
servations of glacial striw on
Hiniwerss Wslands.% 2 cle
Peaeeiase W..and §. 43° W.,
with average general direc-
GLO UDOT. Sere) iajs ow eet 5. 20°W.

FROM NOTES BY Dr. A. C. LAWSON.

Rainy lake, east arm (upon the
international boundary),from
its east-southeast extremity
to Brulé Narrows, twenty-
four localities....... S. 28°-73°° W.

do., East arm, from Brulé Nar-
rows and the Seine river to
the mouth of the lake, forty
NOGRILDIES S| So i50 ot ss. 2 S. 28°-61° W.

Canadian portions of Rainy
lake. with its many bays and
several canoe routes north-
ward, 137 other recorded lo-
GALI DERM aaiseN so ca6.s'6 S. 18°-63°W.

Rainy river, island four miles
above the Manitou rapids.S. 38° W.

do., one mile below the Long
Sault, and at the first and
second rapids of Pine river,
three localities, alike....S$.24° W.

do., one mile above the mouth
Giykud DIG nivel jays S.. 38° W.

FROM NOTES BY Dr. A. C. LAw-
SON{ AND Dr. G. M. DAWSON.§

Around the Lake of the Woods,
observations in about 180 lo-
calities by Dr. Lawson and
assistants, and in about 60 lo-
calities reported by Dr. Daw-
son, ‘‘the great majority”’,i.e.,

SA Per CNUs. sie. S., d0°-0D> Wi. =

but 13 per cent. are..S. 10°-34° W.;

and 5 percent. are...S. 56°-83° W.

Only four localities showed cours-
es more westerly than S. 65° W., as
follows:

On the southeast side of Big
island, striw bearing....S 75° W.
intersect others bearing.S. 37° W.

On the west side of Bigsby is-
land, which, like the preced-
ing, lies near the middle of
Sand Hill lake (the southern
and largest part of the Lake
of the Woods), double sets of
Strize were observed in two
places, respectively
Be ne oy Ws, N. 80° W. and S. 20° W.
PLC asarters N. 83° W. and S. 33° W.

On a point projecting from the
Minnesota shore in the south-
western part of this Sand
Hill lake, strie bear..........

Se as S. 70° W. and 65°W..,
with others....S. 35° and 33° W.;
DIS Owerrsineie ty ch Oe rceeestior soe ove Si 102 3B:

NoTEs BY WARREN UPHAM, 1893.

Vermilion lake, west part of
Pine island, S. W. 4, sec. 34,
T. 63, R. 16, three places.....
R Pa CRE Ate) ck coh at Mates ies S. 15°-20° W.
Tower, near the school house.
RTOS Vie P arcs ailimiefelere octs- eters S. 10° W.
with variation to..S.and S.S. W.
A half mile southwest of Tower
-..5. 5° and 15° E., and S. 10° W.
On the south ridge,close to Tower:
At Lee’s mine, about..... Saylos. Wie
Southeast summit, also about..

*“Report on the Geology of Hunters’ Island and adjacent country,’ Geol. and
Nat. Hist. Survey of Canada, Annual Report, new series, vol. v, for 1890-91.

+Geol. and Nat. Hist. Survey of Canada, Annual Report, vol. iii, for 1887-88.
+Geol. and Nat. Hist. Survey of Canada, Annual Report, new series, vol. i, for 1885.

SReport on the Geology and Resources of the Region in the Vicinity of the Forty-
ninth Parallel, from the Lake of the Woods to the Rocky Mountains, 1875.

38 TWENTY-SECOND ANNUAL REPORT

Southwestern slope of this hill,
several places, about 100 feet
above Tower..Due S.-S. 15° W..,
with rare defiected striz.S. 10° E.

Greenstone knoll, + mile north-
east of Tower Junction, be-
side branch railroad to Sou-
dan, -mosbtly:f- se seeee S.-S. 5° W.;
with other courses. ....-......

S. 15° E., S. 20° W., and S. 35° W.

Soudan, street car depot.......

S. 10°-15° W.

do., southwest edge of village
ierslntata vase sreteee ale seco rere “SHES eu AWE

North ridge, close to Soudan, +
mile west of summit and 30

i a as

feet lower....... S. 20° and 30° W.

also, tew Biri 40-5), ecas oes Ss.
do., at west end of the old

Open Vain: 15 eis, cake S. 15° W.

Jasper peak, three places near
top, each having two sets of
SUIS RLS oes Sa Rees
.-§. 10°-15° W., and S. 30°-35° W.

Ely, many places on top of hill
in village, two slightly vary-
ing sets (the second most
ADUNGAMG) Sam. cae oe Se cee
...9. 20°-25° W., and S. 30°-35° W.

do., + mile farther east, two
courses, both plentiful, inter-
SCCUING MS ck csohe tenes
.-..9. 15-20° W., and S. 45°-50° W.

Hinsdale, close west of D. & I.

R. railroad, several places....
..-5. 10°-20° W., and S. 25°-30° W.
do., above the old quarry,

several places........S. 15°-20° W.

Nearly one mile northwest of
Allen Junction, many strize
in two sets, intersecting.....
eee tet S. 35° W., and S. 50° W.
Allen Junction, two _ places,

abundant........... S. 45°-50° W.
About two miles southeast from
ASU cae selon pide melee S. 30°-35° W.

Close west of railroad 1 mile
south of Little Cloquet river
OL OGs stint! catcieah soto

Rock cut 50 rods long, # mile
north of Two Harbors, nine
places, mostly......... N. 80° W.;
with variations to............

W. and N. 70° W.

Top of hill in S. E. + of sec. 27,

T. 53, R. 11, 14 miles west of
the last, at hight of about 500
feet above lake Superior. N.75° W.

Lighthouse point, + mile south-
east of Two Harbors village,
CWO DIRCES: Haitlencd kale iisk oe aie
...N, 85° W., and (mostly) due W.

Lester Park, at east side of
mouth of Lester river. three
places, mostly...... S. 50°-60° W ;

S. 35° W.

also on same rock surfaces...
..S. 70° W., due W., and S. 30° W.

The magnetic needle is deflected
here to the N. E. and E. N. E., but
these bearings were determined by
comparison with the trend of the
north coast of lake Superior, and
with the direction to elevators in
Duluth, 6 to7 miles distant. All
the following observationsof glacial
strie in and near Duluth likewise
depend not only on compass read-
ings (corrected for average mag-
netic variation, about 10° east of
north), but also on the simultane-
ously observed courses to prominent
buildings or land marks or to the
sun. The needle in numerous
places varied 10° to 60° or more and
occasionally even 180° (pointing to
the south instead of north), on ac-
count of the influence of the mag-
netite-bearing gabbro of this area.
In many other places, however, the
Magnetic courses were nearly cor-
rect.

In Duluth and its vicinity (with fig-
ures in parentheses noting the ap-
proximate hights in feet above lake
Superior):

East Superior street, east end of
rock cut (200), about + mile
northeast from the Endion —
school house (which is at 180
fO6E):s (6 oi sce ooh a oe ee S. 75° -W.

Crest of this cut (250). .... S. 70° W.

+ mile N. KE. from Endion school
house (225).S. 85° W.and S. 40° E.;
both courses being represent-
ed by long and deep, clearly
glacial furrows on asomewhat
weathered rock surface.

20 rods north of this school —
house, at a hight of nearly 50
feet above it (225)..S. 70° W.,
..§. 85° W., due W., and N. 63° W.

A few feet west of last (225)....
aeetst t S. 80° W. and S. 60° W.

Again, about 5 feet farther west
pa MSA. N. 50°, 55°, and 60° W.

50 feet west of last, on a grand-
ly furrowed surface 20 feet
lonoi225).seen eens S. 75°-85° Wis
with broad glacial grooves 4
to + inch deep, from which
any intersecting finer strie
that may once have existed
are lost by weathering.

About 15 rods N. N. W. from
the Endion school house (200),
in two places, mostly.S.80°-85° W.;
also, on the same surfaces....
STR sere Va Cotas ite N. 80°-85° W.

STATE GEOLOGIST. 39

On Woodland avenue (490), about
+ mile south of the Hardy
school house (which is at 510

te ns 2k Satna W.

Near Buena Vista street (450),
# mile east of the great pene
of Chester creek ........ Sao We
14 miles W.S. W. of the dion
school house, near Brewery
creek (425), about 30 rods east
of Piedmont avenue bridge. .
Retariers oes 3. kavaprtrael Peete sie< S. 85° W.
15 rods west from the last, on
ledges in the bed of this prook
(425). W.,N.80° W..and 8.80°-85° W.
About 6 rods S.W. from the last,
at a small quarry (460)..N. 85° W.
Extensive smooth ledges 4+ mile
S. S. E. from the last (425),
mostly effaced by weathering
N. 85° W., due W., and S. 80° W.
Thence, on continuation of these
ledges + mile southward (400-325),
distinct glacial striz were seen in
many places, occasionally accom-
panied with large ‘‘chatter
marks” which are convex east-
ward, respectively in order from
north to south: (1) W.; (2) N. 75°
and 65 °W.; (3) N. 80° W., crossed
by others bearing S. 20° W.,which
curve within an extent of four
feet to a course due S.; (4) S. 50°
Pesto): IN. 807 Ws (6) W.,. 5S. W:,
S., and S. E., all clearly glacial
and crossing on the same surface;
(i). 10° W.: (8) N. 80° W., S. 70°
W., S. 60° W., S. 50° W. and curv-
ing in two feet to S. 30° W.. with
others S. 30° W. and curving in
six inches to S. 10° W., all ona
space of about four feet square,
intercrossed; (9) S. 70°. W., many
parallel striwe, crossed by a few
others, N. 80° W.; (10) S. 70° W.,
Sale (many), and S. 30° K., the
last being surely glacial and ex-
tending straight 3 to 4 feet.
als tract is avout + to? mile
N. W. of the High School
iililaine (which is at 125 feet). ]
On the Boulevard near Third
and Fourth avenues W. (4+
mile S. W. from the forego-
ing) and thence southwest-
erly to the Seventh avenue
inclined railway, striz plenti-
ful in many places (all about

ETEMEEH) oak estes acts S. 50°-60° W.,
with occasional deflections
ORR A Bee S. 75° W. and S. 30° W.

On and near the Boulevard for
a half mile southwest from
the inclined railway, several

places (all about 475 feet),
HIOSHLY <. 2.25.4 oos-4e S. 50°-60° W.,
with deflections to...........
..S. 70° W., S. 85° W., and due W.
Above the Boulevard + to $ mile
N. E. from the inclined rail-
way, many places (525-550)...
S. 70°-80° W.
30 rods W. (555) from the top of
this railway (which is at 535
1925 Dion Aone tees arestia: S. 65° W.
About 15 rods S. W. (575) from
the last..S. 80° W. and N. 80° W.
About 50 rods W. (590) from the
top of the inclined railway .

ee ead

bang ict he eee ete Bee S: 80° W.
+ mile N. W. from this railway
(590-600) .......... S. 85° W.-W.

+ to + mile N. W. from the rail-
way, three places (about 600
feet), successively............ °
(1) N. 75°-80° W.; (2) N. 75° W.;

(3) N. 85° W.

# mile farther N.W., near High-
land Park village (675). N. 75° W.

Piedmont avenue, between
Seventh and Eighth streets
(875), extensive rock expos-
ures, With very distinct gla-
ciation in many places, all...

Re Se Se clea: ane. S. 65°-70° W.

About 4+ mile west of last, close
below the Boulevard, on large
outcrops (425), striz# remain-
ing in many places...........

S. 60°, 65°, 70° and (rarely)80° W..,
crossed in one place by striz

S. 20° E., which curve with-

in 18 inches to 8. 10° H

It is noteworthy that such curv-
ing striz, seen elsewhere in twenty
places or more, are in all cases de-
flected to more southward courses,
when traced forward as the ice cur-
rents moved. At this locality the
curving marks are rather broad and
deep gouges, far more so than any
of the prevailing W.S. W. striz.

Fifth avenue W. (at hight of
about 300 feet), 20 rods west
of the Institute of the Sacred
Heart, mostly...... S. 55°-65° W.;
crossed by a few deep elaciys
AUTOS G: ota lesa sean S. 2

Lake shore, 10 to 15 rods N. .
from mouth of Chester creek,
strie most abundant...S. 50° W.;
also common, 8. 60° W.; with
a few deflections to..........
YO EE S. 30° W. and S. 70° W.

Lake shore, about 30 rods S. W.
from Chester creek ..........
S. 40° W., S. 55° W. and S. 70° W.

40 TWEN'TY-SECOND

Superior street 4+ mile N.E.
from the city hall and public
library (40), several places,
SHORING. © ..3 30s «Se seme S. 60° W
With; OUbeTS.-: \.'} c+ pee eee

wee ee

Michigan street, near Twelfth

avenue W. (50)...... sien a WN

do., between Fourteenth and
Fifteenth avenues (28) Ae ake?
do, within + mile 8S. W. from
the last (at hight of 20-30 feet)
to Garfield avenue (which
leads over Rice’s point to

West Superior), mostly.S. 40° W.

but intersected by...........

ener ree ew eee

In West Duluth.

At quarry about 4 mile N. E.
from the Longfellow school
Howse (75).o au eee can. 5S.

10 rods W. of last (100).........

About 15 rods farther W. N. W.
(100) 2 cz wav Nood teeta: S.6
4 mile north of the foregoing,
on the D., M. & N. railway
near Fourth avenue W. (175)
15 rods E. of last, at the inter-
section of this railway and
State street (175)...N. 80°-

In Carlton and its vicinity.
Thomson, 15-20 rods S. E. of

thes depotasise sess N. 80° W.

3 to 6 ae east of the last.....

Thomson daw. 2... .22 N. 70° W.

Beside the St. P. & D. railroad
+ mile west of St. Louis river,

c mostly Pak iy pisiciote Rete ade Ns 0°. 9

inpersected. by.s.:-21- Se. wee oe
Bees N. 55°-60° W. and N. 80° W.
About 15 rods west of the last,
mostly
with others, equally distinct,
crossing on the same surface
<2) O02 Wey

ee ee

Northeast edge of Carlton vil-
lage, on street leading to
IENOMSON”, seca ties

S. 45° W., and S. 70°-80° W.

S. 65° W. and due W.

10° WY.

68° W.

S. 75°-80° W.

85° W.

N. 52°-55° W.

N. 80° W.;

SS, SGOT) WV s5,0os a es
S. 20° K. and S. 30° E.

6 FIN. CUI «

ANNUAL REPORT

The very prominent and plenti-
ful slate outcrops at and near Car)-
ton, and northward to Cloquet,
have almost completely lost their
glacial marks by weathering. In
searching several hours, both at
Carlton and Cloquet, I was unable
to find any strie surely referable to
glaciation.

Close north of the N. P. rail-
road about 1 mile west of
Carlton, a few glacial striz..
soya bis eres S. 50°, 55° and 65° W.

Within 14 miles southedastward
from Carlton the N. P. railroad has
five rock cuts, at four of which I
searched in vain for glacial marks.
The fifth cut, however, about 30
rods long and 15 feet deep, 14 miles
from Carlton, shows on the recently
uncovered slate of its edges at each
side of the railroad very interesting
glacial strie, as follows:

On the southwest side, near the
northwest endof the cut.....

N. 65° W., and N. 45° W.

Two rods S. E. from the last,

plentiful striv......... N. 45° W.
Again, two rods fartherS. E.,

abundanmtiess. sce e eae S. 80°

intersected) Dy.:): =.= sk eee
S. 15° W., due S., and S, 45° E
each of these courses being
represented by only two or
three glacial gouges.
About three rods farther S. E.,

many very Clear strig@..... due W
25 feet onward S. E...S. 85° W.,

and partly S. 80° W. and due W.

The same westward striation is
also well shown on this southwest
side of the cut in other places with-
in two rods southeastward.

On the northeast side, at the.
crest of the cut, about 10 rods

S. E. from the last, plentiful

Be. calas ered alos eee a N. 80° W.;
crossed by pat glacial gouges
bf dee tceeld S., S. 20° E., and S. 45° E.

These cross mee are two to
six inches long, numerous.
About 25 feet N. W. from the
last, the well preserved main
striation is......... -S. 85° W;
crossed by a few short glacial |
marks..... S. 20° E., and S. 45° E.

STATE GEOLOGIST. 41

Deflections of Glacial Currents.

During the time of maximum extent and thickness of the ice-
sheet, its currents doubtless flowed southward upon all the
northerr part of Minnesota, but with considerable variation
on one side to the west and on the other to the east of due
south. In the region bordering lake Superior, and thence
south and southwest to the Mississippi, the currents were
turned southwesterly, for the driftless area of Wisconsin,
whose margin extends also into southeastern Minnesota, indi-
cates that the glacial outflow from the western part of the lake
Superior basin moved in a curving course successively to the
southwest, south, and east of south, in its passage through
Minnesota. Uniting with this flow the more western part of
the ice-sheet above the Manitoba lake region and the Red river
valley moved nearly due south as the axial portion of the great
ice-lobe which stretched across Minnesota and Iowa, becoming
at the culmination of the Glacial period confluent south of the
driftless area with the ice that moved southwestward from the
region of lakes Michigan, Huron, and Erie. During the depar-
ture of the ice-sheet, however, when its latest currents were
recorded by the strive which remain for our inspection, the in-
equalities in the rates of melting of different portions of the
retreating ice border shaped it often into minor lobes and deep
embayments, very unlike its outlines at the time of greatest
extent, and continually changing in form as the process of the
melting and recession pushed the ice boundary back. In gen-
eral this retreat was from south to north, but the courses of
the moraine belts show that on some tracts it was from west
to east, and less frequently, at least in this state, from east to
west. Everywhere the outermost few miles of the vanishing
ice-sheet had its currents turned strongly toward its boundary,
since on that side there was a steep slope of the ice surfaée.

In the vicinity of Duluth, where the foregoing notes show an
unsurpassed complexity of divergent and intersecting glacial
striz, we may generally refer the courses between S. 30° W.
and S. 60° W., inclusive, to the main current of the ice-sheet
here previous to any great deflections by the irregularities of
the final melting. Occasionally, however, local southward de-.
flections were doubtless of much later date, being due to inden-
tations of perhaps only a few rods extent in the retreating ice
border. The more common directions, ranging from S. 70° W..
to W. and N. 80°-70° W., belong to the time of glacial recession

42 TWENTY-SECOND ANNUAL REPORT

and imply that the withdrawal of the ice boundary here was
from west to east.

Similar westward defiections of the glacial currents crossing -

the shores and islands of the Lake of the Woods and on the
Big fork of Rainy river are likewise referable to the closing
stages of the glaciation. When the ice was thickest and dur-
ing its retreat nearly to this region, the currents of ice flow
from the area of Paleozoic limestones west of the Lake of the
Woods and lake Winnipeg passed south and southeast, carrying
their limestone drift to the mouth of Rainy lake and the basin
of the Big fork, becoming there or close eastward confluent
with the ice flow from the north and northeast, which over-
spread all of the country north of lake Superior. But during
the recession of the ice the laving action of lake Agassiz ap-
pears to have caused exceptionally rapid melting along the
Red river valley and upon the whole area covered by this gla-
cial lake east to the Big fork, so that the ice currents there
were shifted from southeastward to westward and even north-
westward courses, being turned toward the open and lower
lake expanse. In a former report,* I supposed these striz on
the Big fork to represent an increasing eastward deflection of
the previous southeasterly current; butit now seems to me more
reasonable, from consideration of the courses of moraines and
of the extent of lake Agassiz in northern Minnesota, to attrib-
ute their deflection to the somewhat earlier melting of the ice
from the part of the lake Agassiz area crossed by the Rainy
river than from the upper part of the Big fork basin, whereby
the latest ice currents on the Deer river and contiguous parts
of the Big fork were almost reversed from their former direc-
tion.

The changes in the directions of the ice-flow near Duluth
were more remarkable in their abundant evidence by glacial
striz than I have anywhere else found; but observations com-
parable with these were recorded on the quartzyte ridge in
Cottonwood county, southwestern Minnesota,+ and I have seen
almost equally interesting and plentiful deflected glacial strize
in Somerville, Mass.t It is also to be noted that the overlap-
ping of northeastern drift by northwestern drift in Wright
county, Minnesota, and thence eastward to the St. Croix river

*Geol. and Nat. Hist. Surv. of Canada, Annual Report, new series, vol. iy, for 1888-89,
pp. 119, 120 E.

*Geology of Minnesota (Final Report), vol.i, pp. 503-505.

+tProe., Boston Society of Natural History, vol. xxvi, pp. 33-42, March 15, 1893.

STATE GEOLOGIST. 43

on the boundary of Wisconsin,§ proves for that large district
during the closing stages of the Glacial period a reversal of the
direction of glacial currents far more extended in space and
time and more important in their deposition of drift than in
the Big fork district.

TIEL.

Unstratified glacial drift, called till, or boulder-clay, which
was laid down directly by the ice-sheet without modification
by water transportation, assorting, and deposition in beds, occu-
pies probably two-thirds, ora larger part, of northeastern Min-
nesota. It consists of boulders, gravel, sand and clay, mingled
indiscriminately together in a very hard and compact forma-
tion, which therefore is frequently called ‘‘hardpan.” In this
part of the state, the boulders of the till are usually so plenti-
ful that they are sprinkled somewhat numerously on its sur-
face; yet there are seldom more, on the large portions of the
- country which are adapted for agriculture, than the farmer
needs to use, after clearing them from his fields, for the found- «
ations of buildings and for walling up his cellar and well.
They are rarely abundant enough to make walls for the en-
closure of the fields, as in New England.

Three kinds of till occur in this region, each being mainly
restricted to its distinct geographic limits; but on the belts
containing their general boundaries, there is often an over-
lapping of one on another, or successive alternations of two
interbedded. Adjoining portions of the ice-sheet have won
and lost once or repeatedly in pushing against each other.

1. On the west, the till brought by the southward and south-
eastward glacial currents contains plentiful boulders, not only
of Archean and Taconic rocks, but also of the Paleozoic
magnesian limestones which are the bed-rocks of a large part
of Manitoba.

2. Over the greater part of the country eastward from the
Big fork, and from Winnebagoshish and Leech lakes, the till
was derived from the north and northeast and contains still
more plentiful Archean and Taconic boulders, as granites,
gneiss, schists, gabbro, quartzyte, slate, etc., while boulders of
limestone are exceedingly rare or altogether absent, their only
source being Paleozoic formations in the basin of James and
Hudson bays.

§Proc., Am. Assoc, for Adv. of Science, vol. xxxii, for 1883, pp. 231-234. Geology of
Minnesota. vol. ii, pp. 254-256, 409-413.

44 TWENTY-SECOND ANNUAL REPORT

3. The third kind of till is that which was brought by the
ice-flow from the lake Superior basin. It is characterized by
comparative scantiness in the supply of granite, gneiss, crys-
talline schist and gabbro boulders, by the absence of limestone,
and by the large proportion of fine detritus of dull reddish
color from the erosion of the Cambrian red sandstones and
shales, and of the partly sedimentary and partly igneous Ke-
weenawan series, which form the shores and bed of lake Supe-
rior. This red till, with few boulders, has its typical develop
ment about Duluth and Superior, and forms the flat expanse
which gradually rises from the west end of lake Superior
along the Nemadji river and the lower part of the St. Louis
river. Thence, with slow decrease of the prevailing deep red-
ness of its color, it extends northward to Biwabik, westward
into the southeastern part of Aitkin county, and southward to
St. Paul and Minneapolis, though on a large region from

southern Pine county nearly to St. Paul, it is covered, as was ,

before noticed, by overlapping northwestern till.

Along the Duluth& Iron Range railroad from Highland station
to the St. Louis river, and in the excavations for working the
Biwabik iron mine, I observed many very interesting sections
of alternating and often interbedded till deposits of the second
and third kinds here described, derived respectively from the
north or northeast and from the basin of lake Superior on the east.
Plate Il shows four of these sections. Though found abundantly
in this belt, such alternating till accumulations, attributable to
changes of glacial currents, are very rarein most drift-bearing
regions. They here belong probably to the time of the final
recession of the ice-sheet, when, as we have seen by the de-
flected courses of striation, its currents were far more liable to
changes than during the previous time of greater extent and
depth, and resulting generally steady flow, of the ice. These
alternations of till deposition seem to me well accordant with
the view which I have elsewhere presented,* that the drift
during its transportation was englacial, and that its deposition,
excepting on a broad marginal portion of the drift sheet, was
chiefly reserved until the time of glacial recession. Much of
the previously englacial drift appears then to have become
amassed beneath the ice as a ground moraine of subglacial till.
Probably in these sections no more than 1 to 3 feet, or at the
most 5 to 10 feet, in the latter case comprising the two upper

*Bulletin, Geol. Soc. of America, vol. v, pp. 71-84, Jan. 1894.

Geol. and Nat. Hist. Sur. Minn. XXII Ann. Rept. PI. II.

Fia@. 1. SECTION ON THE DuLUTH & IRON RANGE RAILROAD, IN THE NORTH PART OF
SEC. 1. T. 54, R. 12, THREE MILES NORTHWEST OF HIGHLAND STATION. Length, 4 mile;
hight, 25 feet.

Fic. 2. SECTION ON THE DULUTH & IRON RANGE RAILROAD, IN THE SOUTH PART OF
THE S. W. 44 OF SEC. 23, T. 55, R. 12, % TO 34 MILE NORTH OF THOMAS SIDING. Length,
4 mile; hight, 6-15 feet.

Fic. 3. SECTION ON THE DuLUTH & IRUN RANGE RAILROAD, IN THE SOUTHEASTERN
PART OF SEC. 15, T. 55. R. 12, TWO AND ONE-HALF MILES SOUTHEAST OF CLOQUET

2 RIVER STATION. Length. 44 mile; hight, 20 feet.
‘

Fig. 4. SECTION OF PART OF THE WEST SIDE OF THE BIWABIK IRON Mine, OCT. 18,
1893; SHOWING IN THE BASAL PART OF THE DRIFT TWO LARGE MASSES OF THE RED
IRON ORE WHICH WERE GLACIALLY UPLIFTED AND PROBABLY TRANSPORTED VERY
SHORT DISTANCES. Length of section, 150 feet; hight of drift above the ore deposit, 15 to
25 feet.

A. Till of yellowish gray color, but bluish at considerable depths, containing plen-
tiful and often very abundant boulders, derived from the north and northeast.

B. Till of somewhat reddish gray color, containing few or often rare boulders, de-
rived from the east.

STATE GEOLOGIST. 45°

layers of the till, can have remained as englacial and finally
superglacial drift when the ice boundary was withdrawn across
this area.

RETREATAL MORAINES.

Northeastern Minnesota is crossed by several belts of knolly
and hilly till, with far more abundant ‘boulders than are found
on its more extensive comparatively smooth tracts. These
belts of somewhat thicker, more rocky, and prevailingly ridged
drift were accumulated along the border of the’ ice-sheet dur-
ing stages of halt or slight reiidvance interrupting its general
retreat at the close of the Glacial period. Wherever the
vicissitudes of the wavering climate caused the chiefly waning
border to remain nearly stationary during several years the
outflow of the ice to its melting steep frontal slope brought
much drift which had been englacial and on account of the
ablation had largely become superglacial, being exposed on
the surface of the departing ice-sheet. As these marginal ac-
cumulations of drift record the position of the terminal line of
the ice-sheet when they were formed, the name terminal mor-
‘aines has been usually applied to them, but they also may be
called, perhaps more properly, retreatal or recessional mo-
raines.

Four moraine belts have been traced in the part of Minne-
sota northwest of lake Superior, and another, lying next south
and formed before any considerable part of the area of this
lake was uncovered from the ice-sheet, is also included in the
following descriptions. In their order from south to north,
these are the Fergus Falls, Leaf Hills, Itasca, Mesabi, and
Vermilion moraines, being the eighth to the twelfth and most
northern in the series of moraines whose courses have been
mapped in this state. A map showing these moraines, the di-
rections of glacial striz, the areal distribution of the glacial
and modified drift, and the extent of the glacial lake Agassiz
‘in northern Minnesota, forms Plate I, facing page 18, at the
beginning of this chapter.*

Fergus Falls Moraine.
A belt of morainic drift, chiefly till with many boulders,
amassed in hills and irregular ridges 50 to 100 feet above the

*On a smaller scale, the courses of the moraines and other features of the glacial
geology of the entirestate of Minnesota are mapped in Wright’s ‘‘Ice Age in North
America,” 1889, p.546. They areshown in detail for the southern half of the State by
the maps in volumes Iand II of the Final Report of thisSurvey. Many details of
their mapping and correlation throughout the northern half of Minnesota remain
yet to be supplied.

» 46 TWENTY-SECOND ANNUAL REPORT

intervening hollows and frequent lakelets, enters Aitkin county
at the northwest side of Mille Lacs. Thence it extends with a
width of five to ten miles northward to Cedar lake and to the
lakes surrounding Deerwood in Crow Wing county, having in
this part an unusual expansion and probably marking a north-
westwardly re-entrant angle of the ice-border. Passing from
Farm Island and Cedar lakes eastward, the moraine has a width
of about five miles. In the southern part of this hilly belt lie
Hanging Kettle, Diamond, and Mud lakes, the northern part of
Elm Island lake, and Cranberry, Rabbit, Long and Dam lakes.
At the northeast corner of Kimberly township the moraine has
a fine development in many bouldery hills upona width of two
or three miles next northwest and north of Portage lake, being
there crossed by the Northern Pacific railroad.

If my correlation is correct, the vicinity of Portage lake be-
longs to a second re-entrant angle, with its apex pointing
northeastward, from which the moraine, mostly less conspicu-
ous, turns back and passes by the east side of Dam lake. forms
high hills south of Sugar lake, and thence approximately coin-

cides with the eastern watershed of Mille Lacs, until in the”
southern edge of Aitkin county it curves around to an east and

northeast course, passing into Pine county as the hilly belt en-
closing the Pine lakes. The series of low drift hills thus traced
is provisionally regarded, in the descriptions of its portions in
Crow Wing and Pine counties*, as the continuation of the Fer-
gus Falls moraine, which is the eighth of the moraines recog-
nized and mapped in their geographic and chronologic succes-
sion, crossing the southern and western part of Minnesota.

In northwestern Pine county this moraine is well developed
from the Pine lakes northeast to the Kettle river; and farther
northeastward I believe that it is represented by a belt of
somewhat hilly drift extending along the east side of the Moose
Horn river in southern Carlton county, through T. 46, R. 19,

and into Mahtowa (T. 47, R. 18); but thence probably it turns.

back from a re-entrant angle of the ice front and runs south-
ward through T. 46, R. 15, and eastward past Oak and Net lakes
in the north edge of Pine county, to cross the state line nearly
on the watershed between the Nemadji and St. Croix basins.
A tract of moderately hilly till which I observed one to three
miles east of Barnum, and its extension southward by Bear,
Hanging Horns, Moose Horn, Long, and Moose lakes, belong

*Final Report. vol. ii, pp. 605, 642.

+ ota

STATE GEOLOGIST. 47

to this looped morainic belt; and another portion, consisting
partially of till with a somewhat rolling surface, but in larger
part of low kame-like accumulations of sand and gravel, is
crossed by the Great Northern railway in its first three miles
southwest of Holyoke.

Such correlation of these morainic tracts seems to be harmo-
nious with the course of the outer moraines in northwestern
Wisconsin west and north of the driftless area, as mapped by:
Chamberlin.+ It also accords well with the directions of gla-
cial striz found very abundant and distinct on the plentiful

rock outcrops in the vicinity of Carlton, Thomson, Duluth, and

Two Harbors, which, as before noted, run prevailingly west- .
southwestward, but in very many places also display wide de-
flections to the southwest and south and to the west and even
north-northwest. The divergent and variable glacial currents
by which these striz were made doubtless belonged mostly to
the time of recession of the ice border across that district. We
thus learn that the rapidly wasting ice in its departure from
the western end of the lake Superior basin had a definitely
lobate front similar to the looped course assigned to this mo-
raine in Aitkin, Carlton, and Pine counties. Between the
times of formation of the eighth and ninth or Fergus Falls and
Leaf Hills moraines, as these names are here used, the area of
these extraordinary divergent and often intersecting striz was
uncovered by the glacial retreat.
Leaf Hills Moraine.

The next halt or reiidvance of the chiefly receding ice-border
was at the belt of prevailingly knolly and ridged and in part
prominently hilly drift, with many boulders, which extends
from the west side of Gull lake, in southern Cass county, north-
eastward past White Fish lake in northwestern Crow Wing
county, aad north of lake Washburn in eastern Cass county, to
Hill or Poquodenaw lake and ‘‘mountain” (an especially prom-
inent morainic hill which rises about 250 feet above the sur-
rounding country), in northwestern Aitkin county. This belt
is probably the representative of the ninth or Leaf Hills mo-
raine, which in Otter Tail county is partially united with the
Fergus Falls moraine, the two together making the conspicu-
ous Leaf hills (or ‘‘mountains,” as they are commonly called),
100 to 350 feet high. Beyond Poquodenaw the moraine has a
low and inconspicuous development east-northeasterly to the

+U. 8. Geol. Survey, Third An. Rep., for 1881-8, Plates xxviii and xxxv.
—4

48 TWENTY-SECOND ANNUAL REPORT

Mississippi river; but near the east bank of the river, about a
mile north of Aitkin county, it again forms a high hill, known
to lumbermen and log-drivers as the ‘‘Grub Pile,” in the south-
east part of sec. 25, T. 53, R. 24, rising about 200 feet above
the river.

From this hill as the apex of a re-entrant angle of the ice-
sheet, the moraine turns back and extends nearly twenty miles
southward to Sandy lake. Along the first six miles of this
course it is mainly covered by level or only moderately undu-
lating stratified drift, but in the south edge of T. 52, R. 23, it

rises very prominently in Bald bluff, close east of the Missis- —

sippi, and in a series of irregular hills continuing thence east-
ward through the south part of secs. 33 and 34 of this township
and the north edge of secs. 4 and 3, T. 51, R. 23. The crests
of these hills are 150 to 200 feet or more above the Mississippi,
and afford a wide view, the Poquodenaw hill being visible
about fifteen miles distant on the west, and the hills of the
tenth or Itasca moraine, bordering Pokegama lake, twenty
miles away at the northwest. Moraite hills 75 to 150 feet high
stretch from Bald bluff southward along the east side of the
Mississippi to Sandy lake. Thence this belt, lower and less
distinct, consisting partly of kame-like deposits of modified
drift and partly of till, curving southeastward, makes the
shores and islands of Sandy lake and bounds the northeastern
arm of Rice lake, beyond which it passes eastward by Round
and Big Island lakes and through T. 49, R. 22, where its low
swells, hillocks, and ridges project only 20 to 40 feet above the
many tamarack swamps.

Eastward from Aitkin county this moraine is narrowly and
scantily developed in the northwest corner of Carlton county,
but becomes more prominent and broader in the vicinity of
Prairie lake, beyond which, as I am informed by Mr. J. E.
Spurr, its hills and ridges occupy a width of five to six miles
along the south side of the St. Louis river to Stony Brook
and Nagonab. Curving northward beyond the St. Louis, it
borders both sides of the Cloquet river for several miles, pass-
ing northwest of Grand lake. The same belt probably contin-
ues east-northeast to a morainic tract, observed by Mr. A D.
Meeds, adjoining the Cloquet river and Island and Boulder
lakes in the southern third of T. 53, R. 14, and to the narrow
but typically hilly moxvaine which is crossed by the Duluth &
Iron Range railroad a mile north of Highland station. It is
supposed to reach the north shore of lake Superior about mid-

STATE GEOLOGIST. 49

way between Duluth and Pigeon point. Its course beyond
Highland station, however, has been definitely ascertained for
only about thirty miles. Along this extent, passing east-
northeast to the middle of the east side of T. 57, R. 8, the
moraine has been mapped by Mr. Arthur H. Elftman in his
exploration for this Survey during the summer and autumn of
1893, who reports it admirably represented by a belt of very
irregular drift hills from a half mile to two miles wide, with
summits 50 to 75 feet above the land on each side.

Itasca Moraine.

Extending eastward from Jake Itasca, this tenth moraine at-
tains a grand development along the south side of Leech lake,
being there about ten miles wide. In the southern half of its
width it encloses Ten Mile and Fourteen Mile lakes, and Woman,
Wabado and Little Boy lakes. Thence it continues east-north-
easterly across Itasca county, where its abundant knolls and
hillocks of drift, as described by Prof. G. E. Culver in another
part of this report, lie on the northern slope of a high Creta-
ceous ridge in T. 54, R. 26, cover much of the lower country
bordering the shores of Pokegama lake within the next ten
miles, occupy considerable tracts a few miles north and east of
Grand Rapids (attaining a maximum altitude of 300 feet), and
reach from near the falls of the Prairie river east-northeast
past the Diamond iron mine and along the watershed between
the Prairie and Swan rivers to Hibbing.

Along the next thirty miles, to the Embarras lakes, Mr.
Spurr’s descriptions and mapping indicate that the Itasca and
Mesabi moraines are united in a belt mostly two to three miles
wide, which coincides closely with the granite ridge known as
the Mesabi or Giant’s range. Hast of the gap in this range
through which the Embarras river flows (expanding along the
greater part of its valley in a series of beautiful lakes), both
these moraines veer to the south of the granite ridge. . On the
Duluth & Iron Range railroad the exceedingly knolly and con-
fusedly ridged but low belt of the Itasca moraine, strewn with
a countless profusion of boulders of all sizes up to ten feet in
diameter, is crossed from about a half mile to two and a half
miles northwest of St. Louis River station. For observation of
the rough contour and abundant boulders which are usually the
two chief characteristics of these retreatal moraines, I know of
no other more impressive view than is seen here from the pass-
ing train, although none of the elevations rise more than 50 or

50 TWENTY-SECOND ANNUAL REPORT

75 feet above the adjoining tamarack swamps and the plentiful
bowl-like hollows which are enclosed by the morainie accumu-
lations.

In Lake county the moraine varies from one to two or three
miles in width, and crosses ranges XI to VIII (the belt of Mr.
Elftman’s exploration in 1893) along the line dividing T's. 59
and 60. His descriptions show that the moraine along this ex-
tent of twenty-four miles is typically developed in very irregu-
lar low hills and ridges, mostly between 50 and 75 feet in hight.
Hight to ten miles farther on, taking an east-northeast course,
its hills of drift, heavily covered with white pine, are reported
by Mr. H. V. Winchell as surrounding lake Harriet, at the head
of the Isabelle river, with ridges of very abundant boulders
close northward. Its course thence eastward to the coast of
lake Superior, which it may reach in the vicinity of Grand
Marais or near the mouth of Brulé river, has not been traced.

Mesabi Moraine.

The most northwestern of the morainic tracts in Minnesota
which are here correlated together as the Mesabi or eleventh
moraine lies between the south and north divisions of Red lake
and consists of a high till ridge, with many boulders, some two
miles wide and extending about ten miles east from the Nar-
rows, with a continuous altitude 150 to 200 feet above the lake.
- Forty to fifty miles southeast from this tract, lower drift hills,
referred to the same moraine, border the north side of lake
Winnebagoshish, and reach thence southeastward to Deer and
Bass lakes, near which they occasionally rise to hights of about
200 feet above the general level. Along a distance of twenty
miles to the north from the last named lakes, Prof. Culver re-
ports irregular groups and short series of drift hills, mostly
less than 100 feet high, which seem to represent the complex
accumulations of a re-entrant angle of the ice-border. From
Spider, Trout and Wabano lakes, this moraine passes eastward,
and appears to be merged with the Itasca moraine to form a
compound hilly belt along the Mesabi range from close north
of Hibbing to the upper Embarras lake northeast of Biwabik.
At Mesaba station on the Duluth & Iron Range railroad, and
within a mile southeastward, this Mesabi moraine comprises.
many hillocks and short ridges 20 to 40 or 50 feet high. Thence
continuing northeast, it is represented by characteristic knolly
and hilly drift deposits and abundant boulders on the south side
of the western part of Birch lake, and through the northern

ren

STATE GEOLOGIST. 51

part of Ts. 60 in Rs. XI to VIII, where it is mapped by Mr.
Elftman, lying two to five miles north of the Itasca moraine,
and occupying a width of one to two miles. It probably comes
down to the lake Superior shore about 70 miles farther east,
in the Pigeon River Indian reservation, passing thence beneath
the lake level.

Vermilion Moraine.

A twelfth moraine, named from Vermilion lake, along whose
southern side itis well exhibited, as also south of Pelican and
Net lakes, was first carefully studied and mapped during my
field work in 18938. The portion of its course which I have
examined reaches about 40 miles, from the west extremity of
Vermilion lake east-southeast to Tower and thence east-north-
east to Ely. In total, its whole extent yet known is nearly 75
miles, beginning at the west on the south side of Net lake,
where Mr. C. L. Chase, engaged during the past summer in
government township surveys, reports a belt of irregularly
grouped drift hills, 50 to 100 feet high, with very abundant
boulders. Next south of Pelican lake it occupies a width of one
to two miles, and it averages about one mile wide in its course
skirting the southern shores of Vermilion lake for the distance
of twenty miles from its west end to Tower. This belt in most
portions is distinguished more by its wonderful profusion of
boulders, ranging in size up to 5 or 6 feet and occasionally 10 or
15 feet in diameter, than by its large amount of drift amassed
in hillocks and ridges. Its multitudes of noulders strow the
surface of the Tower town site, and are conspicuously piled
upon the southern slope of the high rock hill called the South
ridge, just north of this town; but they are absent from the top
of this ridge and from its northern slope, which are chiefly
bare rock. Turning northeasterly for the next one and a half
miles, this moraine thinly caps the North ridge at Soudan,
above its iron mines. Thence it runs to the east and skirts
the northern and eastern base of Jasper peak, which, like the
top of the ridge near Tower, has almost no drift.

Six to ten miles farther east, this belt is crossed by the Duluth
& Iron Range railroad, on which its bouldery drift knolls and
ridges are cut through in many places within two miles west
and an equal distance east of Robinson Lake station. At Ely
its boulders are very abundant in and near the village. Less
than a mile to the south, associated with the morainic belt, is
an irregular esker ridge ot sand and gravel, often very coarse,

52 TWENTY-SECOND ANNUAL REPORT h

trending from west to east and here and there expanding into
small plateaus, with altitudes mostly 50 to 75 feet above the
railroad and iron mines. Four to seven miles east of Ely,
plentiful low drift hills, with many boulders, were observed by
Mr. Elftman adjoining the north end of White Iron lake, south-
east of Garden or Eve lake, and north of Farm lake. The ex-
tent of this belt beyond its limits as here described remains
unexplored; but it is doubtless traceable west at least to the
area of lake Agassiz, and much farther eastward.

Although this morainic belt is very distinct and certainly
records a nearly stationary stage interrupting the retreat of
the ice-sheet, I estimate its volume of drift added above the
average of the surrounding region to be only 5 to 10 feet on its
variable width of a half mile to two miles. A half, or at least
a third, of this added volume consists of boulders from six
inches to ten feet in diameter.

For the region of Ely and Vermilion lake I estimated the
volume of all the drift thus: bare ledges of rock, with no drift
or too little to be worth consideration, about a tenth of all the
surface; ledges thinly drift covered, probably four-tenths, with
an average of about 5 feet of drift; while the remaining half of
the country, having diverse deposits of sand and gravel, re-
treatal moraines, or smoother tracts of till, may have an aver-
age depth of 40 feet of drift. By this estimate the mean thick-
ness of the drift there, if uniformly spread, would be about 22
feet.

V.—MODIFIED DRIFT.

The deposits included under this title are waterworn and
stratified gravel, sand and clay or silt, which were washed
away from the drift upon and beneath the retreating ice-
sheet by the streams due to its melting and to accompanying
rains. Kames, eskers, sand and gravel plateaus and
plains, the valley drift (varying from very coarse gravel
to very fine loess and clay, often eroded so that its remnants
form terraces), are the principal phases of the modified drift.
In being derived directly from the ice-sheet, these deposits
had the same origin as the glacial drift forming the common
till and the greater part of the retreatal moraines; but they
were modified, being separated from the coarser portions,
further pulverized or rounded, and assorted in layers, by
water. .

STATE GEOLOGIST. 53

Kames and Eskers.

Associated with the tillin the moraines, a considerable part
of these accumulations of marginal drift often consists of
irregularly stratified gravel and sand in knolls and short, ir-
regular ridges, which are called kames. Such stratified de-
posits are also occasionally found on the generai till expanse
between the morainic belts. In both situations they are at-
tributable to deposition by small streams descending from the
melting surface of the ice-sheet, being accumulated in the
short cafion-like gorges which were melted into the ice-border
at their mouths. The slackening of the steep and rapid de-
scent of the streams there emerging upon the land in front of
the ice caused them to deposit the coarser part of their load
of gravel, sand, and clay, which was left in these hillocks and
ridges when tne enclosing ice-walls melted away.

Plateaus of gravel and sand, deposited similarly as kames
but fillmg broader indentations of the retreating ice-front,
have a considerable development in the vicinity of Sandy lake,
with altitudes 50 to 75 feet above the lake level. They also
occur west of Carlton and close southeast of Cloquet, and in
numerous other localities. Within one to two miles south of
White Iron lake, they are described by Mr. Elftman as form-
ing flat-topped hills about 100 feet high.

Eskers, which are also the deposits of glacial streams but
differ from kames in forming prolonged, narrow ridges, a half
mile to one mile or sometimes several or many miles in extent,
are infrequent in this state. Only a few examples have been
noted in the large northeastern region which is here reported,
and none has been traced along a distance of more than one or

two miles.
Valley Drift and Plains.

Moderately “undulating or nearly level tracts of sand and
gravel, spread on the land in front of the retreating ice-sheet
by streams which had gathered this modified drift from the
melting ice surface, are found extensively developed in Wadena,
Hubbard, Cass, Crow Wing, and St. Louis counties, and to less
degree in many other portions of northeastern Minnesota.
Areas reaching ten to twenty mi#es on each side of the Crow
Wing, Pine, and St. Louis rivers, consist of these plains, often
bearing chiefly jack pine (Pinus banksiana), but in their more
rolling and ridgy portions also commonly bearing the red or
Norway pine. Where these lands are very moist, lying only a
few feet above the stream courses, and especially, as in parts

54 TWENTY-SEGOND ANNUAL REPORT

of the St. Louis basin described by Mr. Spurr, where thin de-
posits of till are spread like a veneer above the modified drift,
the larger and more valuable white pine grows. The soil pre-
ferred by this tree, however, is the till or boulder-clay, which
generally rises higher than these areas of modified drift and
bears a heavy growth of hardwood (species of poplar, birch,
oak, elm, ash, maple, basswood, and other deciduous trees),
wterspersed with white pine, sometimes only seen here and
there as scattered trees, but frequently occurring in small or
large groves, from a few rods to several miles in extent.

VI. THE WESTERN SUPERIOR GLACIAL LAKE. AND THE LATER GLACIAL
LAKES WARREN AND ALGONQUIN, |

If the courses of the Fergus Falls and Leaf Hills moraines
are rightly traced as noted in the foregoing pages, the earliest
outlet from the Western Superior glacial lake, held by the bar-
rier of the waning ice-sheet still occupying the central and
eastern part of that lake basin, probably flowed across the di-
vide between the head streams of the Bois Brulé and St. Croix
rivers, where a remarkable eroded channel is found.* The in-
dentation of the ice-front north of the Wisconsin driftless area

at the time of formation of the first or Altamont moraine points -

decisively to the melting backward of a great re-entrant angle
in the ice boundary upon the country between Duluth and Ash-
land, including the place of the Bois Brulé-St. Croix outlet, at
atime previous to the melting of the ice upon the district
reaching west from that outlet to Aitkin county. The correla-
tions of retreatal moraines given here and in the second volume
of the Final Report imply the probable beginning of existence
of the Western Superior ice-dammed lake between the times of
formation of the seventh and eighth or Dovre and Fergus Falls
moraines. But after the accumulation of the latter and before
the time of the next or Leaf Hills moraine, the ice-melting in
the western portion of the lake Superior basin and thence west
to the Mississippi river was very rapid, so that the greater
part of Aitkin county, the whole of Carlton county, and the
country from Duluth north to Grand, Wild Rice, and Island
lakes, and from T'wo Harbogs north to Highland station, were
uncovered from the departing ice-sheet. According to the
probable duration of the glacial lake Agassiz, estimated to
have been only about 1,000 yearst, in which the stage between
*Geology of Minnesota, Final Report, vol. ii, pp. 642, 643.

*+Geol. and Nat. Hist. Survey of Canada, An. Rep., new series, vol. iv, for 1888-89, pp-
50, 51 E.

ae. %"

> *

STATE GEOLOGIST. 5D

the Fergus Falls and Leaf Hills moraines was a small fraction,

this retreat of the ice from Aitkin and Carlton counties and the

west end of lake Superior appears to have occupied no more
than a century or perhaps only half a century.

The old channel of outflow to the St. Croix river has a width
of about a fifth of a mile in its narrowest place. Its bed is
1,070 feet above the sea, or 468 feet above lake Superior; and
it is bordered by bluffs about 75 feet high, showing that when
the course of outflow began here the Western Superior glacial
lake was about 550 feet above the present lake level. Proba-
bly the highest part of the swamp now forming the watershed
in the channel has been filled twenty to twenty-five feet since
the lake forsook this mouth, which was thus lowered by ero-
sion some 100 feet, from 1,150 to 1,050 feet, approximately,
above the present sea level. Beaches and deitas referable to
this glacial lake are found, as described by Dr. A. C. Lawson,*
in Duluth and its vicinity and on Mt. Josephine, near Grand
Portage, showing that the lake while outflowing to the St.
Croix had been extended, by the recession of the ice-sheet,
along all the northwestern shore of lake Superior in Minne-
sota; but it may well be doubted whether it continued far into
Canadian territory. Before the recession of the ice-sheet had
uncovered the country about Port Arthur and farther east-

‘ward, probably its departure from Wisconsin and Michigan

had. permitted the glacial representatives of lakes Superior and
Michigan to become confluent over the low divide of the Au
Train and Whitefish rivers, the latter of which is tributary to
the Little bay de Noc. The Western Superior glacial lake,
suddenly falling about 60 feet, as is shown by the hights of
successive beaches and deltas, then became merged in the gla-
cial lake Warren,+ outflowing at Chicago to the Des Plaines
and Illinois rivers.t

Dr. Lawson, in his report before cited, has not discriminated
between the traces of the earlier lake outflowing 1o the St.

*“Sketch of the Coastal Topography of the North Side of Lake Superior, with Special
Reference to the Abandoned Strands of Luke Warren,” Minnesota Geol. Survey,
Twentieth An. Rep., for 1891, pp. 181-289, with map, profiles,and figures from photo-
grapbs.

t+tNamed by Prof. J. W. Spencer in honor of Gen. G. K. Warren, Science, vol. xi, p. 49,
Jan. 27,1888; Proc. A. A. A.S., vol. xxxvii, for 1888, pp. 197-199; Trans., Roy. Soe. of
Canada, vol. vii, for 1889, sec. iv. p. 122.

+For my former discussions of the later stages of the glacial lakes and retreat of
the ice-sheet in the St. Lawrence basin, see “Glacial Lakes in Canada,’’ Bulletin,
Geol. Soc. of America, vol. ii. for 1890, pp. 243-276; and “Relationship of the Glacial
Lakes Warren, Algonquin, Iroquois and Hudson-Champlain,” Ibid., vol. iii, for 1891,
pp. 484-487.

56 TWENTY-SEGOND ANNUAL REPORT

Croix and those of lake Warren; but this seems desirable for
convenience and definiteness in description and discussion.
Many small glacial lakes, and a few as here attaining large
size, became finally merged, by the retreat of the ice, in the
single vast expanse of lake Warren, which stretched from Du-
luth eastward and southeastward to the west end of the basin
of lake Ontario, covering the whole or the greater part of the

four higher Laurentian lakes. In the western part of the lake ~

Superior basin the ancient high shore lines, with their evi-
dences of wave erosion and deposition, belong, from hights
(above the present lake) of 450 or 475 feet up to 607 feet, the
highest observed by Dr. Lawson, to the Western Superior lake.

Below these hights, the numerous lower shores mark succes-

sive stages of lake Warren, which were due only in very
slight measure to erosion of its outlet, but which the present
writer confidently believes to have been caused almost entirely
by a progressive uplift of this region, elevating the northern
and northeastern parts of the area of the great glacial lake,
while its outlet and some southwestern portions of its area
remained with little or no change of hight.

A quite different view is given by Dr. Lawson, who thinks ©

that lake Warren was not held in by the retreating ice-sheet,
but by land barriers, the country on the south and east having

been relatively higher than now, and that the differential sub- —

sidence of the land there and contemporaneous uplifting of the
country about Hudson bay went forward without disturbance
of the horizontality of the old shore lines enclosing lake Sup-
erior. On the west, however, I have ascertained for the south-
ern half of the area of the glacial lake Agassiz, in the basin of
the Red river and of lake Winnipeg, that it experienced a dif-
ferential uplift increasing about one foot to the mile from south
to north during the departure of the ice-sheet. On the east,
Mr. Frank Leverett has demonstrated that the beaches of lake
Warren south of lake Erie were contemporaneous with the
accumulation of adjacent moraines;* and the basin of lake
Iroquois, the glacial expansion of lake Ontario, according to
levelling by Gilbert and Spencer, has been uplifted like that of
lake Agassiz, but with a greater northward ascent of the old
Iroquois beach, amounting to five feet per mile for fifty miles
from Rome to near Watertown, N. Y. It seems therefore im-
probable, in the first place, that lake Warren occupied a land-

*Am. Journ. of Science, IIT, vol. xliii, pp. 281-301, with maps, April, 1892.

STATE GHOLOGIST. 57

locked instead of an ice-dammed basin, and, secondly, that
these recent differential epeirogenict movements on each side
failed to extend across the area of lake Superior.

The great Pleistocene lakes Agassiz, Warren, Algonquin,
and Iroquois, were probably due alike to the barrier of the
waning ice sheet; and their basins appear to have shared ina
general epeirogenic uplift of the whole drift-bearing area of
our continent, when it was relieved from its ice burden. Under
this view, the highest shores at Duluth and on Mt. Josephine
seem readily referable to an ice-dammed lake in the western
part of the Superior basin outflowing in the eroded channel at
the head of the St. Croix river, from which there is an ascent
of about 140 feet in a distance of 120 miles northeast to the 607
feet shore terrace noted by Lawson on Mt. Josephine. Later,
for the earliest and highest stage of lake Warren, likewise ice-
dammed, with outlet to the Mississippi across the low divide
at Chicago, about 595 feet above the sea, we have now an as-
cent of 420 feet in about 350 miles to the highest shore found
by Lawson near the Sault Ste. Marie, at a hight of 414 feet
above lake Superior. The differential uplifts thus indicated
for both of these old lake shores are similar in their vertical
amount and geographic extent with the fully known epeiro-
genic uplift of the lake Agassiz area.

BEACHES.

The upper limit of lacustrine action in Duluth and its vicinity
is marked by discontinuous beach deposits on the upper part of
the steeply ascending bluffs at an altitude of 535 feet to 540 feet
above the lake. In the recess between two projections of rock at
the top of the Seventh Avenue inclined railway, where the hight
of this shore was determined by Dr. Lawson, it appears as a small
terrace of sand and fine and coarse gravel, 12 to 15 rods long and
about 5 rods wide. The verge of its flat surface is on the level
of the railway station floor, and thence the terrace rises
four or five feet to where it adjoins the till and rock slopes.
In front the same gravel and sand fall off about 20 feet within
a few rods, and then spread out again in a similar lower and
longer terrace, eight to ten rods wide, with its surface gently
inclining lakeward at 515 to 505 feet, approximately. These

+The terms epeirogeny and epeirogenic (continent-producing, from the Greek epeiros,
a mainland or continent) are proposed by Mr. G. K. Gilbert (in “Lake Bonneville,”
Monograph I, U.8.Geol. Survey, 1890, p. 340), to designate the broad movements of up-
lift and subsidence which affect the whole or large portions of continental areas and
of the oceanic basins.

58 TWENTY-SECOND ANNUAL REPORT

deposits were brought partially by inflowing waters from
above, being so far of delta character, and partially by shore
currents from wave erosion of the adjoining bluffs on each side,
being for such portion more strictly beach accumulations.
They mark stages of the Western Superior lake when its mean
levels here were about 535 and 510 or 515 feet above lake
Superior.

Next below these shore lines is the most definite and persist-
ent beach of the entire series, both of the Western Superior
lake and the ensuing lake Warren. This was generally repre-
sented along the bluff face by a narrow beach terrace or slight
shelf, less steep than the slopes below and above it, so that its
contour line, 470 to 475 feet above the present lake, has been
used as the course of a driveway, known as ‘‘the boulevard,”
which has been graded and is much used for pleasure driving,
along an extent of four miles, above the principal part of the
city of Duluth, from Miller's creek to Chester creek. Beyond
these limits the boulevard is planned to be extended for dis-
tances of four miles more, both to the southwest and northeast,
following the same altitude and shore line, giving a total length
of twelve miles. Its hight is only a few feet above the water
divide in the old channel of outflow from the Western Superior

lake to the St. Croix; but, if we make due allowance for the

partial filling of that channel with postglacial alluvium and
peaty swamp deposits, it seems probable that this latest shore
of that glacial lake has now an ascent of 15 or 20 feet in the
distance of about 25 miles from its outlet north-northwest to
Duluth. The earlier and higher shores here were made when
the erosion of the outlet lacked successively about 65 and 30 or
35 feet of its final depth; but a certain part of its earliest ero-
sion had been done before the retreat of the ice extended the
lake to this northwest coast. ‘These three beaches of the Wes-
tern Superior lake may be conveniently designated as the First
and Second Duluth beaches and the Boulevard beach.

Between the neighborhood of Duluth and Mt. Josephine, no
definite observations of the Western Superior glacial lake shore
lines have been obtained, although there can be no doubt that
they extend continuous along this distance, which is about 130

miles in a nearly direct northeastward course. When the —

woods of this high coast shall be cleared off, as will probably
sometime be done in many places for farming and pasturage,
the beach levels will be observed, especially the highest and
lowest of the three noted at Duluth. Attempting to correlate

t
RO ee) nw vay eee

STATE GEOLOGIST. 59

these beaches with those found by Lawson on Mt. Josephine,
LT identify the 535 feet and 510 to 515 feet Duluth shores as
respectively his 607 and 587 feet shores; and the 475 to 470 feet
beach of the Duluth boulevard becomes apparently the con-
spicuous 509 feet beach of Mt. Josephine. The total different-
ial uplifting of the two upper shores between these localities
has been about 70 feet, of which about half had been accom-
plished previous to the time of the Boulevard beach. This pro-
gressive uplifting of the land soon after the recession of the
ice, while indeed the ice barrier yet remained in the eastern
part of this lake basin, is in full parallelism with the epeirogenic
movements which gave their northward ascents to the beaches
of lakes Agassiz and Iroquois, and, as Prof. J. W.Spencer and
Mr. F.. B. Taylor have shown, to the beaches of various por-
tions of lakes Warren and Algonquin.

During the past season’s field work I obtained numerous
observations of the beaches of the Western Superior lake near
Thomson, and between Carlton and Wrenshall, some 15 miles
southwest of Duluth, and in the vicinity of Holyoke, a station
of the Great Northern railway, 15 miles south of Carlton. Near
Holyoke, which is about 30 miles west of the outlet at the head
of the Bois Brulé and St. Croix rivers, the successive lake
levels indicated by the beach ridges observed and provision-
ally referred to the Western Superior lake are about 520, 500,
and 455 feet above lake Superior, corresponding well with the
slightly inclined planes of the Duluth and Mt. Josephine shores,
and indicating a lowest water surface of about 455 feet at the
outlet.

Hight beaches of lake Warren, mostly on the same levels
with its well defined deltas, were also observed in the vicinity
of Duluth, on the Northern Pacific railroad from West Superior
to Wrenshall, and on the Great Northern railway to the vicin-
ity of Rhodes’ Mill, four miles northeast of Holyoke. The
highest three of these shore lines bear conspicuous deposits of
beach sand and gravel which are cut by the railroad, the first
being one and a half miles southeast of Wrenshall, the second
nearly a mile farther east, and the third close west of Barker
station, about a half mile east from the last. The altitudes of
their crests at the railroad cuts are respectively 427, 401, and
361 feet above lake Superior; and the mean water levels of
lake Warren while these deposits were being accumulated
appear to have been approximately at 410, 385, and 350 feet,
Of these the first, which was the highest level of lake Warren,

60 TWENTY SECOND ANNUAL REPORT

held during only a very short stage, is represented by the
fourth in the series of deltas of Chester creek in Duluth; and
the second and third have their representation in the fifth of
those deltas, while apparently the second is the Nelson
beach, and the third the McEwen beach, of Mr. F. B. Taylor’s
observations along the south side of lake Superior, north of
lake Huron, and in the vicinity of lake Nipissing.* The Nelson
beach, generally marking the highest well defined shore of
lake Warren, is 410 feet above lake Superior at Houghton,
Michigan; 414 feet near the Sault Ste. Marie; and 538 feet, or
1,140 feet above the sea, near North Bay, lake Nipissing. The
McEwen beach, supposed to have been formed when lake War-
ren at Duluth stood about 350 feet above lake Superior, is
identified as the 365 feet shore terrace at Ste. Marie, while
near lake Nipissing its hight from the same plane is 488 feet,
being 1,090 feet above the sea level. In Dr. Lawson’s series
of observations, the higher and earlier shore of 410 to 415 feet
near Wrenshall and at Duluth seems to be probably represented
by the 440 to 458 feet plain and terrace at Grand Portage,
and by the 455 feet terrace of an old delta plain on the Kamini-
stiquia river; and near lake Nipissing, according to my correla-
tion with Mr. Taylor’s notes, it is found about 1,205 to 1,220
feet above the sea.

To present concisely the results of my studies of the whole
series of lake shores observed by me at and near Duluth, in
their probable correlations with the shores observed farther
eastward by Dr. Lawson, Mr. Taylor, and Prof. Spencer,t
notes of the twelve lake levels found here are successively pre-
sented as follows, in descending order, their altitudes being
given in feet above lake Superior. On northern portions of
the lake Superior coast several of these seem to be each repre-
sented by two or more shores, separated by distinct vertical
intervals of 10 feet or more. Most of the beaches, it should be
remarked, are very feebly developed, even in the most favora-
ble situations for their formation, and are not discernible along
the far greater part of all the lake borders. During all the
time of uplifting of the basin and sinking of the water surface

by its finding successively lower outlets and by their erosion -

*Bulletin, Geol. Soc. Americs, vol. v, pp. 620-626, with maps, April, 1894. Am. Geolo-
gist, vol. xiii, p. 220, March, 1894; and 316-327 and 365-383. with maps, May and June,
1894. Am. Jour. Sci., III, vol. xliii, pp. 210-218, March, 1892.

+J. W. Spencer, Am. Jour. Sci., III, vol. xli. pp. 12-21, with map, Jan., 1891; same vol.,
pp. 201-211, with map, March, 1891, Bulletin, Geol. Soc. of America. vol. ii, pp. 465-476,
with map, April, 1891.

et toy Poe

y wes
" nee

STATE GEOLOGIST. 61

from higher to lower levels, whenever the diminishing lacus-
trine area was nearly unchanged for a few years or longer, the
erosion and deposition effected by the great waves of storms,
and the tribute of streams forming deltas, recorded these shore
lines.

BEACHES OF THE WESTERN SUPERIOR GLACIAL LAKE.

First Duiuth beach: at Duluth, 535 feet above lake Superior; on Mt.
Josephine, 607 feet; at Kimball, Wis., 570 feet; at L’Anse and Marquette,
Mich.. about 590 feet.

Second Duluth beach: at Duluth, 510 or 515 feet; on Mt. Josephine, 587
feet.

Boulevard beach: at Duluth, 470-475 feet; on Mt. Josephine, 509 feet.

BEACHES OF THE GLACIAL LAKE WARREN.

Belmore beach (name given by Prof. N. H. Winchell to the corresponding
earliest shore line of lake Warren in Ohiot): near Wrenshall and in Du-
luth, 410-415 feet; at Grand Portage, 440 feet; on the Kaministiquia river,
455 feet; at Mackenzie, on the Canadian Pacific railway 13 miles north-
east of Port Arthur, Dr. Lawson’s descriptions indicate that this lake
level, at about 475 feet, adjoined the melting ice-sheet (1. c., p. 264);
eight miles east of Cartier, about 600; southeast of lake Nipissing, 605-620.
The “Ridgeway beach” of Prof. Spencer.

Nelson beach (named by Taylor in the vicinity of North Bay, lake Nipis-
sing; probably united with the Belmore beach in Ohio and northward to
Mackinac island): at Duluth, 385 feet; at Mackenzie, a morainic terrace,
420 feet; at Jackfish bay, 418; Sault Ste. Marie, 414; Houghton, 410; North
Bay, 538. The “Algonquin beach” of Mr. Taylor on Mackinac island, at
185 feet; near Petoskey, about 80 feet; and at Traverse City, 60 feet. The
hights (likewise above lake Superior) of this shore about Green bay of
lake Michigan are noted by Mr. Taylor as follows: at Green Bay, 0; six
miles north of Menominee, 30 feet; South Bay hill, 115 feet; Cook’s Mill,
near the head of Big bay de Noc, 150 feet.

McEwen beach (named by Taylor near North Bay): at Duluth, 350 feet;
Schreiber and Terrace bay, 391-2; Sault Ste. Marie, 365; North Bay, 488.

Thibeault beach (also named by Taylor near North Bay): Great Northern
railway, about 23 miles northeast of Foxboro, 290-300 feet; Mt. Josephine,
313; Mackenzie, 327; Sault Ste. Marie, 311.

Double Bay beach: at Duluth, 255-260 feet; at Double bay, 279 feet; on
Isle Royalet, about 270; Carp river, 288.

First Beaver Bay beach: at Duluth, 155-160 feet; at Beaver bay, 173 feet:
eastward represented by two beaches:—a, at Grand Portage, 232 feet: at
Carp river and Pie island, 222; at Terrace bay, 243; at Sault Ste. Marie,
224; on the Keweenaw peninsula, 220;—b, at Mazokamah, 214; Terrace bay,
228: Dog river, 216; Sault Ste. Marie, 208; on the Keweenaw peninsula
(Taylor and Lane), about 200.

tProc. Am. Assoc. for Adv. of Sci., vol. xxi, for 1872, pp. 171-179. Geology of Ohio, vol.
ii, 1874, pp. 56, 418, 433.

+Altitudes of this and other lower shore lines on Isle Royale are kindly supplied by
Dr. A. C. Lane, from unpublished observations for the Geol. Survey of Michigan.

62 TWENTY-SECOND ANNUAL REPORT

Second and Third Beaver Bay beaches (becoming three northeastward):

at Duluth, 85-90 feet: Beaver bay, 126 and 115; Pigeon river (third), 134; _

Isle Royale, about 130; shore above Carp river, 164, 128, and 122; Port
Arthur (third), 149: Silver Islet, 168, 161; 149; Jackfish bay, 176, 158: Sault
Ste. Marie, 150; Keweenaw peninsula, 170, 150, 145-125 (delta of Huron
creek, A. C. Lane).

Chester Creek beach: at Duluth, 45-50 feet; Beaver bay, 80: Isle Royale, 90;
McKellar’s point, 101; Port Arthur, 118; Nipigon, 132; Montreal river, 135;
Mamainse, 122.

BEACH OF THE GLACIAL LAKE ALGONQUIN.

Algonquin beach (named by Prof. Spencer, in Proc. A. A. A. S., vol. —

xxxvii, p 199): at Duluth, united with the present lake beaches; at Beaver
bay, 20 feet; Good Harbor bay, 27; Grand Portage, 38; McKellar’s point,
48; Carp river, 52; Pie island, 43; Port Arthur, Nipigon, and Montreal
river, 61; Sault Ste. Marie, 49; Houghton and Marquette, about 25; near
Algoma, 60-80: near North Bay, on lake Nipissing, 140. The Nipissing
beach of Mr. F. B. Taylor; but not his ‘‘Algonquin beach” on Mackinac
island (Am. Jour. Sci., III, vol. xliii, pp. 210-218), which is the highest of
the Jake Warren shores, being apparently the compound representative
of the Belmore and Nelson beaches.

The front of the departing ice-sheet was the barrier of the
Western Superior glacial lake while the one receded and the
other advanced from Duluth northeastward to Mt. Josephine
and the most northeastern point of Minnesota, and eastward
to Marquette. When the farther glacial recession opened the
space for this lake and the similarly expanding lake Warren
to be merged together above the low land of the eastern part
of the Michigan upper peninsula, the Western Superior waters
fell about 60 feet below their former outlet to the St. Croix,
and thenceforward the outlet of lake Warren past Chicago
carried away the drainage from the glacial meltiag and rainfall
of the Superior basin. Ata time that was probably somewhat
later than the end of the Western Superior lake, its analogue,
the Western Erie glacial lake, which had outflowed past Ft.
Wayne, Indiana, to the Wabash, Ohio, and Mississppi rivers,
became likewise lowered and merged in lake Warren, which in
its soon ensuing maximum stage stretched from the south end
of lake Michigan to the north side of lake Superior, northeast
to lake Nipissing, and eastward to the east end of lake Hrie
and the southwestern limits of the lake Ontario basin. While
the outlet continued at Chicago, all the northern part of the area
of lake Warren, extending about 600 miles from Duluth to lake
Nipissing, was uplifted hundreds of feet.

The uplifting was approximately uniform for this entire ex-
tent, and indeed for the whole width of the Superior basin,

STATE GEOLOGIST. 63

reaching 150 miles from south to north; so that the present
altitudes of the elevated beaches, while somewhat inclined, are
yet through long distances so nearly horizontal that they par-
tially and in a remarkable degree justify Dr. Lawson’s opinion
that the ancient lake levels remain parallel with that of to-day.
The sum of all the epeirogenic movements since the formation
of the Belmore and Nelson heaches, along a nearly due north
line measures as follows, in comparison with the Chicago out-
let: from Chicago for about 185 miles north to the southern
end of Green bay, very little, the old shore still being nearly
unchanged; about the north end of Green bay, at the head of
the Big bay de Noc, 150 feet; at Houghton, on the Keweenaw
peninsula, 410 feet; and at the north side of lake Superior, 420
feet, or more probably 475 feet. Along a west to east belt 50
to 100 miles wide, including the upper peninsula of Michigan,
the rate of differential uplifting ranged from one to five feet
per mile from south to north; while on a large area farther
north there was little differential movement, but in general a
surprisingly uniform and regular elevation of the lake Super-
ior district.

When the glacial melting and retreat at length permitted
an outflow from the St. Lawrence basin over a lower pass,
which was through central New York to the Mohawk and Hud-
son, the water surface of the basins of lakes Michigan, Huron,
and Superior, fell only some 50 or 75 feet, from the latest and
lowest stage of lake Warren to its short-lived successor, lake
Algonquin. This lake was ice-dammed only at low places on
its east end, as at or near the heads of the Trent and Mattawa
rivers, lying respectively east of lakes Simcoe and Nipissing,
where otherwise its waters must have been somewhat further
lowered to outflow by those passes. A careful study of the
late glacial epeirogenic uplifting of all portions of the St.
Lawrence drainage area, as known by the present inclinations
of its many shore lines, convinces me that Gilbert* and Wrightt
have overestimated the importance of the outflow, if any such
took place, from lake Algonquin past the present lake Nipis-
sing to the Mattawa and Ottawa rivers. Professor Spencer’s
Algonquin beach is very clearly the Nipissing beach of Mr.

*Proc. Am. Assoc. for Adv. of Science, vol. xxxv, for 1876, pp. 222, 223. “The History
of the Niagara River,” Sixth An. Rep. of the Commissioners of the State Reservation
at Niagara, for the year 1879, pp. 61-84, with maps and sections (also in the Smithsonian

An. Rep. for 1890, pp. 231-257).

+Bulletin, Geol. Soc. of America, vol. iv, pp. 423-5; with ensuing discussion by Dr.
Robert Bell, pp. 425-7.
-—5

64 TWENTY-SECOND ANNUAL REPORT

Taylor; and this earliest and principal stage of lake Algonquin
is shown by these beaches to have coincided closely in area
with lakes Michigan and Superior, but to have been consider-
ably more extensive eastward than the present lake Huron and
Georgian bay. It held a level which now by subsequent dif-
ferential epeirogenic movements is left probably wholly below
the present level of lake Michigan by a vertical amount rang-
ing from almost nothing to about 40 feet. Its shores were
nearly coimcident with the western shore of lake Huron, but
eastward they are now elevated mostly 150 to 200 feet above
that lake and Georgian bay; and in the lake Superior basin
they vary from about 50 feet above lake Superior at its mouth,
and along its northeastern and northern shores, to 25 feet at
Houghton, and to a few feet or none at Duluth. The earliest
outflow of lake Algonquin doubtless passed southward by the
present course of the St. Clair and Detroit rivers; thence it ran
east asa glacial River Erie, following the lowest part of the
shallow bed of the present lake Erie, which then had an east-
ward descent of probably 200 feet, allowing no lake or only a
very small one to exist in the deepest depression of the basin;
and north of Buffalo it coincided with the course of the Niagara
river.

The Niagara gorge has since been eroded by the recession
of its waterfall; and the outflow from the upper Laurentian
lakes has been constantly pouring over the receding cataract,
excepting possibly (but improbably) that it may have been
diverted for some very short time, as less than a century, to
the Mattawa. It seems to me far more probable that the
epeirogenic uplift of the Nipissing region, which had elevated
it about 450 feet during the existence of lake Warren, con-
tinued so fast that both the Trent and Nipissing—Mattawa
passes were raised above the level of lake Algonquin before
the glacial retreat uncovered the country east of them so that
outlets could be obtained there.

With the continuance of the uplift of the lake Superior ba-
sin after the formation of the Algonquin beach, the mouth of
lake Superior and the Sault Ste. Marie came into existence;
and this movement allowed the lake level at Duluth to fall pro-
bably 40 or 50 feet beneath the Algonquin and present shore
line. Subsequent differential elevation of the eastern and
northern parts of the basin, as compared with Duluth, has
again brought the west end of the lake up to the Algonquin
shore; but not until the St. Louis river, while the water surface

STATE GEOLOGIST. 65

stood considerably lower than now, had deeply eroded its
broad channel through the very gently sloping expanse of till
from Fond du Lac to the harbor of Duluth and Superior.

lt would be very interesting to trace the relationship of the
epeirogenic uplifting of the lake Warren basin with those of the
contemporaneous lake Agassiz on the west and the slightly
later lake Iroquois on the east, but the limits and scope of
the present report forbid this. Nor can we here consider
what these glacial lakes teach concerning the recession of the
ice-sheet from New York and New England, which are thus
clearly shown to have been the last portion of the United
States, at least eastward from the Rocky mountains, to be un-
covered from the fast waning continental glacier. The re-
treatal moraines of all the drift-bearing area east of the great
angle of the drift boundary insouthwestern New York appear,
in the light of these studies, to be somewhat (though not many
hundreds of years) newer than all the series of moraines with-
in the limits of the United States west from that angle to Min-
nesota and North Dakota.

DELTAS.

Not only the St. Louis river, but also many small streams in
the vicinity of Duluth, brought noteworthy deltas of gravel
and sand into the formerly much higher glacial lakes which
represented lake Superior. The largest delta plain which I ob-
served reaches about a mile eastward from the St. Louis river
at Thomson and has an altitude of 455 to 460 feet above the
present lake. It was probably formed nearly at the old lake
level or within a few feet below it, contemporaneous with the
formation of the Boulevard beach. Still water deposits, laid
down at ashort distance off shore, swept by the prevailing
winds and shore currents southward from the mouth of the St.
Louis, as it then was, are now found as the beds of stratified
clay worked for brick-making at and near Wrenshall, three to
four miles south of this delta. Numerous other sand and ©
gravel deltas of the St. Louis, mostly of small extent, will
doubtless be easily recognized by adequate search; and the cor-
responding finer silts borne southward thinly cover many
tracts of the wooded Nemadji drainage area, above its much
greater thickness of till.

On Tischer’s creek, in the northeastern suburbs of Duluth,
large terrace remnants of a delta which was brought in during
the stage of the First Duluth beach are found at 540 to 550 feet,

66 TWENTY-SECOND ANNUAL REPORT

about a quarter to a third of a mile north of the Hardy School.
Other and lower deltas of this stream lie west of this school
house and within a quarter of a mile south.

The most interesting series of deltas, however, which I ex-
amined in Duluth is situated along the course of Chester creek.
Besides its present course, this creek sent a part of its waters
into the Western Superior glacial lake by a more western chan-
nel, occupied by a very small brook, there depositing the con-
spicuous gravel and sand banks above and below the boule-
vard a half mile southwest of Chester creek, which are now
being extensively excavated by the city street department and
in part for use as masons’ sand. Along Chester creek I noted
nine successive delta terraces or small plains, usually well rep-
resented on each side of the creek, which has cut deeply
through them to the underlying rock or steep till slope. In
their descending order, these have the following altitudes:

1. About 540 to 530 feet; belonging to the First Duluth stage.

2. About 510 to 490 feet; representing the Second Duluth beach,

3. At 480 to 460 feet; deposited during the time of the Boulevard lake
level.

4. At 420 to 410 feet; the Belmore level.

5. From 380 to 350 feet; representing together the Nelson and McEwen
beaches. :

6. From 260 to 230 feet, including the former site of the Forest Hill
cemetery; the Double Bay beach. (Probablyadelta deposit may be found
nearly midway between the last two, at the Thibeault shore line.)

7. At 160 to 150 feet; on the first Beaver Bay shore line.

8. At 90 to 75 feet; corresponding to the Second and Third Beaver Bay
beaches.

9. At 50 to 45 feet, close to the mouth of this creek, and rising imme-
diately on the north side of the Duluth & Iron Range railroad. From
this delta is derived the name of the Chester Creek beach.

After examining this series of deltas and mapping their locations, the
altitudes here noted were obtained from a large scale contoured map of
Duluth in the office of Mr. D. A. Reed, the city engineer.

; Se ee
oe

ets

IV.

PRELIMINARY REPORT OF FIELD WORK DUR-
ING 1893 IN NORTHEASTERN MINNESOTA.

BY ULYSSES SHERMAN GRANT.

CONTENTS.
Page
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Te aRPR MR IKCC OR Vy atl serie s yonis. hoist efor vc sav aybielfe ciltiSta Aus oi cpateol syavenatane tere 2 70
Mt; . lron-bearing-rocksiof Akeley lake: . 2i..0 52... 52 ens «cise cele 72
RM ee eT ATA NTIS Fo yes, alt aso:ctay tye 25.07 epic dels evateerprmpelcte ays 6, aerere 73
NEPA Steet roe aia creo rois ata ch w arecalte hal y af acaeens Tisralalsaayere wlohats,onate 73
EEHICKMESSANG GIVISTONS: 2c ccastaiassielore sie afslolsversisis level eysts/ore 74
The upper, or graywacke-slate, member.......... 74
The middle, or black slate, member.............. 74
The lower, or iron-bearing, member.............. 74
ME NEGUS TOC Foie alte rattie Si cio cieynin, vie isie oes Noumas, ols Sins clyeuele, «fla 76
VEO IRE We CHA Will: 2 sei ah oe sia chao sais -¥ decisions cu ¥v ao 76
CUE PLO CS cats ai ates oh lelece tel ele al Fa ee teats’ win lelei an nioieners 76
ADVTS PLATE GGA ITO. soa 2'm 0s, aTecet sls nels ale\a, coi phd salma s,c78 "= uy
PACA ETAL GU WES 3 cterhicle cient ateiel io elaySo eo ch alos0 ote s 40s, otmcei hiera wheta 77
ITINERARY.

During the last week in June and the first in July the writer
accompanied Prof. N. H. Winchell on a trip along the north
shore of lake Superior from Grand Marais to the end of Pigeon
point and return. Quite a number of the more important locali-
ties along this shore were examined, an account of which will
be given by Prof. Winchell. After returning to Grand Marais
another trip of ten days was made northward and northwest-
ward, by what is known as the ‘‘Iron trail,” to Brulé lake and

68 TWENTY-SECOND ANNUAL REPORT

thence to Gunflint lake, where a week was spent in examining
the iron-bearing rocks in T. 65-4.* In the first part of August
the writer participated in the excursion of the Geological
Society of America through the mining regions of Michigan.
On returning to the field in the last part of August the region
of Gunflint lake and that west, south and east of this lake was
examined, and data were obtained for a geological map of this
region. This work continued until the early part of October,
when a few days were spent in company with Messrs. N. H. and
H. V. Winchell in visiting some of the critical exposures near
Tower.
MAPPING ACCOMPLISHED.

At the beginning of the season the writer was assigned that
part of Minnesota lying in ranges 2-7 west of the Fourth prin-
cipal meridian to map geologically and topographically. Of
course it was impossible, with the time and assistance allowed,
to cover all this area (over 1500 square miles) much more care-
fully than already had been done; consequently that part lying
between T. 63 and lake Superior was neglected and the work
was concentrated on the rest of the area.

The part of the Mesabi range in this portion of the state was
divided into three divisions (plates), in which more detailed
work was done than on the rest of the region, and in each di-
vision the vicinity of the outcrop of the iron bearing rocks re-
ceived more attention than the rest of the plate. These plates
and their approximate areas are as follows:

Plate 80.—Ts. 63-64, Rs. 6-7; 144 square miles; Fraser Lake plate.
Plate 81.—Ts. 64-65, Rs. 4-5; 143 square miles; Akeley Lake plate.
Plate 82.—Ts. 64-65, Rs. 2-3; 101 square miles; Gunflint Lake plate.

The amount of mapping accomplished is outlined in the two
following sections.

I, TOPOGRAPHY.

This part of the work was done under the direction of the
writer by Messrs. C. P. Berkey, L. A. Ogaard and Alex. N. Win-
chell. Mr. Berkey, who was in charge of this work during
July and August, was in the field from June 26th to September
2d;+ Mr. Winchell from June 26th to August 26th; Mr. Ogaard
from June 26th to October 5th, but during September and
October considerable of his time was devoted to other duties.

The altitudes of all the principal lakes, and of a large num-

*[n this paper the “Range” is always west of the Fourth principal meridian.

+Mr. Berkey has written an account of his work on the topography, which
appears later in this volume.

STATE GEOLOGIST. 69

ber of the smaller ones, were ascertained accurately by level-
ling from lake Superior.* By means of aneroid barometers and
hand levels data were obtained for the drawing of contour
lines, which are fifty feet apart. The topographical work on
that part of the Mesabi range mapped by the above mentioned
party is much more accurate than that done by parties of the
survey further west, for two reasons; first, the levels of the
lakes were accurately determined, and second, these lakes were
used as checks on the aneroids every few hours. The results
of the work of 1893 and that of the writer for 1892 are as fol-
lows: :

Piate 80.—Levels of most of the lakes by barometrical read-
ings; location of the prominent hills; very little accurate con-
touring. This, however, is an unimportant sheet.

Plate 81.—Practically complete, excepting some of the
northwestern part.

Plate 82.—Practically complete.

In the region south of these plates, except in the vicinity
of Brulé and Ida Belle lakes where the contouring is nearly
complete, very few data have been obtained. To the north of
these plates the levels of almost all the lakes are known,
mostly by aneroid readings, and some contouring has been
done. The hights of the lakes between Gabemichigama lake
and Ely (by way of Knife and Basswood lakes) were obtained
by level.t

ll. GEOLOGY.

In the mapping of plates 80, 81 and 82 the writer found it
necessary to go over the entire ground anew and depended but
very little on the mapping of former parties of the survey, as
their work was more in the nature of a reconnaissance than of
accurate mapping. In addition to a careful survey of the lake
shores, with very frequent trips inland, nearly all north and
south section lines were followed in the vicinity of the iron-
bearing rocks and the Animikie, and occasionally sections were
crossed one to four times. The mapping done during the last
two seasons and some in 1891 is as follows:

Plate 80.—Practically complete, but less time was devoted to

*The levelling was done by Mr. L. A. Ogaard, assisted by Alex. N. Winchell. The
writer can vouch for the care and accuracy with which this work was done, sometimes
under decidedly embarrassing circumstances.

+The hights of many of the lakes and pointsin the area here reported on can be found
on pages 22-25 of Mr. Warren Upham’s report in this volume; alsoin the report of Mr.
C. P. Berkey.

70 TWENTY-SECOND ANNUAL REPORT

this plate than to the others as it is very largely covered by
gabbro.

Plate 81.—Practically complete.

Plate 82.—Practically complete.

In the region south of these plates, except around Brulé and
Ida Belle lakes and in T. 62-6, nothing has been accomplished
since the publication of the geological map in bulletin number 6.
The mapping of the region north of these plates is practically
complete. Special attention has been given to the vicinity of
Kekequabic lake, of which a map has been published (see the
2ist Ann. Rept.,pl. I),and to the outlines of the Saganaga granite
(see the 20th Ann. Rept., pp. 83-95). The lakes lying between
Ogishke Muncie and Ottertrack lakes have been examined and
work supplementary to that of the former parties of the sur-
vey in this region has been done..

SKETCH OF RESULTS OF GEOLOGICAL WORK.

While opportunity has not been had for a careful examination
of the specimens collected during the last two years, and for
the preparation of a report on this region, still there are some
points, which were brought out by the field work and some lit-
tle study since, that are sufficiently clear to warrant a prelimi-
nary statement of the results reached.

I. THE KEEWATIN.

The lakes south of Ottertrack lake in T. 66-6 and the north
half of T. 65-6 have been examined and the rocks found to be
of the usual Keewatin strata with some areas that consist of
volcanic tuff. Large and beautiful exposures of Ogishke con-
glomerate occur on the shores of the lake in S. W. 4 see.
36, 66-6.

The Keewatin in the northern part of the southern half of
T's. 65-4 and 65-5 is composed almost entirely of greenstone
and greenstone schists. Some of these greenstones show frag-
mental materials and are probably of the nature of volcanic
tuff, while other parts are undoubtedly massive eruptives.

The outlines of the Saganaga granite in Minnesota have been
traced, and abundant evidence has been found to show the
eruptive nature of this granite in the Keewatin rocks. Partof
this evidence has been published* for the western edge of this
granite area, and during the last two years facts pointing the
same way have been noted along the southern edge of this

* U.S. Grant, 20th Ann. Rept., pp. 83-95, 1893. Amer. Geol., vol. x, pp. 4-10, 1892.

STATE GEOLOGIST. TL

granite where it comes in contact with the greenstone. The
proofs of the eruptive nature of the granites of Saganaga, Keke-
quabic and Snowbank lakes and of the Giant’s range have been
stated before by the writer,* and in the case of the Keke-
quabic lake granite the matter has been treated insome detail.t
Mr. J. E. Spurr, who has been at work for the survey on the
Mesabi range west of the Duluth and Iron Range railroad dur-
ing the last summer, also states that there is abundant evidence
.of the intrusive and metamorphosing nature of the granite of
the Giant’s range in that district.

It frequently happens, that, where these granites come in
contact with the surrounding rocks, schists more crystalline
than those of the usual Keewatin occur. To these more crys-
talline and completely crystalline schists the Minnesota survey
has applied the term Vermilion, which is regarded as a synonym
of Dr. A. C. Lawson’s Coutchiching. The Vermilion rocks have
been supposed to occupy a distinct stratigraphical position be-
low and older than the Keewatin. The writer has already
called attention to the fact that in the region of the Kawishiwi
river (T's. 63-9, 63-10 and 63-11 W.) there seem to be good
reasons for not separating the rocks mapped as Vermilion from
the Keewatin.§ During the field work of the past two seasons
additional facts have been collected concerning these more crys-
talline rocks (Vermilion), facts sufficient to justify the state-
ments (1) that the rocks called Vermilion in the region of the
writer’s field work are not necessarily lower in the geological
scale than the Keewatin, but that they occur at various horizons
in the Keewatin, (2) that they are only a more crystalline con-
dition of these same Keewatin rocks, and (3) that they proba-
bly owe their more crystalline nature largely to their close
proximity to areas of intrusive granite. It will be noticed that
the Vermilion rocks as mapped usually occur between areas of
Keewatin and granite; in this connection consult especially
plates 10 and 11 of Bulletin No. 10 and the geological map ac-
companying Bulletin No. 6. And, as stated above, some of
these granite areas are known to be intrusive, and very proba-
bly others not mentioned above are of the same nature. The
gradual transition from the Keewatin to the Vermilion rocks
has been described by Messrs. N. H., A. and H. V. Winchell in

* 20th Ann. Rept., pp. 37-38, etc., 1893.
+2ist Ann. Rept., pp. 37-38, 50-54. 1893.
+ Bull. No. X. p. 2, 1894.

§ 20th Ann. Rep., p. 59, 1893.

72 TWENTY-SECOND ANNUAL REPORT

the more recent and annual reports of the survey and more
especially in Bulletin No. 6. The same conclusions in regard
to the relations and position of the ‘‘Vermilion” rocks of the
western Mesabi iron range were reached independently by Mr.
J. E. Spurrt during the last summer.

It would be unwise to extend these conclusions concerning
the ‘‘Vermilion” rocks in the areas studied by the writer to all
similar rocks in northeastern Minnesota and western Ontario;
but it does not seem improbable that these conclusions will in
the future be found to apply to a large part, if not to the whole,
of the so-called ‘‘Vermilion” rocks of the northeastern part of
this state.

Il. IKON-BEARING ROCKS OF AKELEY LAKE.

These rocks lie upon the Keewatin greenstone to the north
and on the south are overlain by the great gabbro mass. They
extend in a narrow belt from near the center of the N. 4 sec. 27,
65-4, westward nearly to the western edge of the N. 4 sec. 34,
65-5 (a distance of about six and a half miles). West of this
they are met with in a few isolated outcrops near the northern
edge of the gabbro, or included in the gabbro, and at Birch
lake (T. 61-12) apparently the same rocks reach a considerable
development and have been exploited foriron ore. In Ts. 65-4
and 65-5 these rocks outcrop in a belt from 300 to 1300 feet in
width, and the dip varies from almost vertical to 20 degrees
toward the south, the average dip being 45-50 degrees. Where
the belt is the widest the dip averages about 30 degrees; this
would make a thickness of 650 feet, which is probably the maxi-
mum thickness of these beds in the vicinity of Akeley lake.

The iron ore of these rocks is a magnetite, making on the
average a rather low grade bessemer ore, with no titanium.
During 1892 and 1893 considerable work was done by the Gun-
flint Lake Iron Company in sections 28 and 29, 65-4, and a rail-
road was completed from Port Arthur to their headquarters in
sec. 28. A number of test pits have been dug and two shafts
have been sunk, the deeper of these is in the S. HE. N. W. 4
sec. 28; in September, 1893, it had reached a depth of 112 feet.
As yet no ore has been shipped and no bed of any considerable
thickness of clean ore has been encountered, although by sort-
ing by hand a fair quality of ore can be obtained.

Prof. N. H. Winchell considers these rocks to belong to the

+Cf. Bull. 10, p. 2, and the explanations to plates 10-12.

STATE GEOLOGIST. 73

lower part of the Animikie,* while Dr. W. S. Bayley has in-
cluded them in the gabbro.+ In this preliminary report the
origin of these ore-bearing rocks and their relations to the An-
imikie and to the gabbro will not be discussed, (See remarks
concerning the absence of a basal quartzyte at Gunflint lake on
pages 74-75 of this report).

IU. ANIMIKIE.

During the season of 1893 considerable new data were ob-
tained concerning the Animikie rocks in the vicinity of Gunflint
lake, and it is now possible to construct a much better geologi-
cal map of this region than has hitherto been published. {

The Animikie rocks about Gunflint lake have been little dis-
turbed; they dip, with local exceptions, at an angle of 8 to 10
degrees a little east of south. In the immediate vicinity of the
gabbro the dip increases and as the slates disappear under this
rock it occasionally reaches 20 to 30 degrees. On the north
side of the lake, where the lower beds lie upon the older ver-
tical crystallines, there has been some gentle bending of the
later rocks, and in the S. 3 sec. 21, 65-4, is asharp synclinal, on
whose southern side the Animikie slates stand almost vertical.

Faults.

The country is made up of parallel ridges trending east and
west. On the south side of each ridge gentle slopes occur,
but on the north steep, mural descents are seen. The tops
of the ridges are composed of diabase sills, which usually
cap a considerable thickness of slates. This. structure
has given rise to the idea that there has been a series of
monoclinal uplifts along east and west fault lines, the down-
throw occurring on the north side of each fault. While this
idea is very plausible as long as topography alone is concerned,
still it seems to find little or no confirmation in the sequence of
the strata. 'The Animikie rocks, as stated beyond, can be read-
ily divided into three divisions, and each division is well char-
acterized lithologically. Such being the case it would be
a comparatively easy matter to recognize any member if
brought out of its normal position by faulting, but in no in-
stance has the writer been able to do this. There seems to be
good’ evidence that no great faults have occurred, although
minor ones of comparatively small throw may exist.

*16th Ann. Rept., pp. 82-89, 1888. See especially Bulletin No. 6, 1891.

+19th Ann. Rept.. pp. 194-210, 1892. Journ. of Geol, vol. i, p. 694, 1893.

¢The best map yet issued is that by Irving and Van Hise in their work on the Peno-
kee range, 10th Ann. Rept. U.S. Geol. Sur., pl. xlii, 1890; and Mon. XIX, pl. xxxvii,1892.

74 TWENTY-SECOND ANNUAL REPORT

Thickness and divisions.

It is easy to separate the Animikie rocks at Gunflint lake into
three well marked lithological divisions, and perhaps each of
these can be subdivided. Below is given this three fold divi-
sion, with the estimated miximum thickness of each.*

The upper, or graywacke-slate, member.—Composed of black to
gray slates and fine graywackes, with some flinty slates; the
upper part shows coarser detrital matter, and the highest beds
seen are fine grained quartzytes and quartz slates. Thickness
1,900 feet.

The middle, or black slate, member.—Composed largely of black
slates, often very fissile, and apparently carbonaceous. At
the bottom of this member is a distinct division of black to
gray slates which are fine grained, siliceous and often flinty;
they reach a thickness of some 60 feet. They are as distinctly
marked off from the black, carbonaceous slates above as from
the iron-bearing rocks below, and perhaps might be put ina
separate member by themselves, but they seem to be distinctly
differentiated only at the western end of Gunflint lake. Thick-
ness of middle member 1,050 feet.

The lower, or iron-bearing, member.—Composed largely of jas-
pery, actinolitic, siliceous and magnetitic slates, usually quite
thinly laminated, and some beds of cherty carbonate and of
lean iron ore. The presence of thin bands rich in magnetite is
a very characteristic feature of this member. Itis also char-
acterized by greenish to reddish siliceous rocks, often spotted
and forming jaspers; to similar rocks on the western Mesabi
range Mr. H. V. Winchellt has applied the name ‘‘taconyte,”
and Mr. J. E. Spurrt has shown that they were originally com-
posed largely of glauconitic greensands, and that in some
cases the glauconite still remains. Thickness of the lower
member 900 feet.

The quartzyte (Pewabic) and conglomerate found at the base
of the Animikie farther west seem to be entirely lacking in the
vicinity of Gunflint lake. This statement may need a few
words of explanation. The name ‘‘Pewabic quartzyte” was
proposed for, and applied to, the iron-bearing rocks of Akeley

*The lowest of these divisions corresponds to the “iron-bearing member.” and the
middle and upper divisions to the ‘‘upper slate member,” of the geological map of
Gunflint lake published by Irving and Van Hise; loc. cit.

+The Mesabi iron range: 20th Ann. Rept., p. 124, 1893.

#The iron-bearing rocks of the western Mesabi range in Minnesota; Bull. No. 10, 1894.

STATE GEOLOGIST. (5

lake.* Subsequently this term has been applied quite exten-
sively to the quartzyte member at the base of the Animikie on
the western Mesabi range, so that now the term Pewabic usu-
ally refers to this quartzyte, which, however, in the Minnesota
reports has been considered as the equivalent of the iron-bear-
ing rocks of Akeley lake. If the iron-bearing rocks of Akeley
lake are thus put at the base of the Animikie, there seem to
the writer to be serious objections to regarding them as the
basal quartzyte and the equivalent of the quartzyte of the west-
ern Mesabi range. In the absence of anything like a con-
glomeratic base, in the intimate and rapid alternation of bands
of siliceous and ferruginous material, and in other respects
these rocks are closely analogous to certain parts of the iron-
bearing member, and it is to this member that the writer would
refer these rocks, if they belong to the Animikie. Moreover,
in the Gunflint lake region no quartzyte has been found near
the base of the Animikie and in several places the iron-bearing
member has been seen lying directly upon the older crysta!-
line rocks. Consequently it is stated that, so far as known, the
basal quartzyte member is lacking in the vicinity of Gunflint
lake.

As is stated above, the uppermost strata of the Animkie near
Gunflint lake are fine grained quartzyte and quartz slates. This
ificrease of coarser siliceous material in the higher beds of the
Animikie is quite noticeable, and is also especially well shown
in the vicinity of Pigeon point, north coast of lake Superior.
At the latter place these quartzose beds (Wauswaugoning
quartzyte) have been placed at the base of the Animikie in the
recent Minnesota reports.t There seems, however, more rea-
_son for placing the Wauswaugoning quartzyte near the summit
of this series than at its base, and for considering it as the
probable equivalent of the quartzose beds at the top of the An-
imikie as exposed near Gunflint lake.

In the above estimates of the thickness of each member the
diabase sills have been included. Their exact thickness is not
known, but it is roughly estimated at not more than 75 feet for
the lower, 100 feet for the middle, and 250 feet for the upper
member. The following figures then will show the maximum
thickness, in feet, of the Animikie at Gunflint lake, the esti-
mate being based on an average dip of not more than 10 de-

JL ee Saws *
*N. H. Winchell; 16th Ann. Rept., p. 86, 1888.

+See especially the “Table of Pre-Silurian Rocks,” facing p. 4 of the 2ist Ann. Rept.

76 TWENTY-SECOND ANNUAL REPORT

grees, and on the assumption that there are no faults which
would make the apparent thickness greater than the real:
Sediments. Diabase ‘Total.

The upper, or graywacke-slate, member... 1,650 250 1,900
The middle, or black slate, member....... 950 100 1,050
The lower, or iron-bearing, member....... 825 75 900

Pobalsa/ ee see at 3,425 425 3,850

Igneous Rocks.

The igneous rocks of the Animikie, so far as seen by the
writer, are all in the nature of intrusive sills or dikes; no sur-
face eruptions have been recognized, nor has any evidence of
contemporaneous volcanic activity been noted in the vicinity
of Gunflint lake.* These sills are composed of diabase that
varies much in grain, sometimes being very coarse in the cen-
ter of the sills. They make up the characteristic ridges of the
region and, as far as surface extent is concerned, cover per-
haps a third of the area of the Animikie, although their. aggre-
gate thickness is much less than one third that of the whole
series. The largest and most prominent sill is that forming
the highest land between Loon and Gunflint lakes and along
the south shore of South lake; it has a thickness of at least 100
feet.

The sills are not found to extend into the gabbro, nor have
the two rocks been seen in contact. However, the gabbro is
cut by a few dikes of diabase that might be referred to the
same date as the sills. At the time of the gabbro intrusion
the surrounding rocks were probably heated considerably, as
the gabbro is not particularly finer grained at its contact with
the country rocks; but in the case of the sills, even of the
largest ones and those in closest proximity to the gabbro, both
the upper and lower surfaces where seen are exceedingly fine
grained. The relative ages of the two rocks are not definitely
determined from the data thus far obtained about Gunflint lake.

IV. THE KEWEENAWAN.
Gabbro proper.

The great gabbro mass of this region was examined over a
considerable extent of territory, This rock is found to vary
somewhat in mineralogical composition, at times becoming, as
at Little Saganaga lake, almost entirely composed of feldspar,

*This agrees well with the statement of Dr. A. 0. Lawson concerning the absence of
voleanie activity in the Animikie; Bulletin No. 8, p. 29, 1893. He proposes for these
sills the term ‘‘Logan sills,’ Ibid., p. 48.

STATE GEOLOGIST. Ce

thus forming an anorthosyte petrographically similar to those
described by Dr. A. C. Lawson from the north shore of lake
Superior;* again it becomes exceedingly rich in olivine, this
mineral sometimes making up half the rock mass.+ The gabbro
was found to include fragments of the Animikie slates, and it
also was found directly overlying and in contact with beds of the
upper member of the Animikie. This gives additional proof of
the post-Animikie age of the gabbro.

Fine grained gabbro.

Associated with the coarse grained gabbro, or gabbro
proper, and more frequently seen near its northern limit, are
finer grained rocks which vary from gabbros and olivine gab-
bros to norytes and olivine norytes. ‘To these rocks the term
‘“‘muscovado”’t has been applied. They are basic igneous rocks
‘and are, as a rule, at least slightly older than the main mass of
the gabbro, which is seen cutting and including fragments of
them.

Acid eruptives.

In Ts. 62-6, 63-5, 63-4, 63-3 and in the southern edge of T.
64-2 are extensive exposures of reddish, hornblendic, granitic
rocks. These make the highest hills of this region and these
hills often form the water divide between the St. Lawrence
and Hudson bay drainage. These rocks are undoubtedly part
of what Prof. R. D. Irving termed the augite syenites of the
Keweenawan,§ but as yet the writer has found no augite in
them; however, in most specimens examined the original na-
ture of the ferro-magnesian constituent cannot be determined.
They probably represent deep-seated parts of the magmas that
produced the extensive flows of rhyolytes, now largely apo-
rhyolytes, || and other acid lavas seen about the Minnesota coast
of lake Superior, especially at the Great Palisades and also at
other points along this shore.

On approaching one of these areas of granitic rocks from the
north afew small acid dikes are seen in the gabbro. These
increase in frequency and size on coming nearer to the central

*Bulletin No. 8, 1893.

+For a description of the gabbro of Minnesota see article by Dr. W. S. Bayley, Jour,
of Geol. vol i, pp. 688-716, 1893.

#See “Remarks on the so-called muscovadyte or muscovado rock,” 2ist Ann. Rept.,
pp. 143-153, 1893. Also Ibid., p.30. 17th Ann. Rept., pp. 130-131.

§Copper-Bearing Rocks of Lake Superior, Mon. V, U.S. Geol. Survey. 1883.

iFor use of this term see article by Dr. Florence Bascom, Jour. of Geol., vol. 1,
pp. 813-832, 1893.

78 TWENTY-SECOND ANNUAL REPORT

mass of granite, and at the edge of this mass apophyses can
be traced directly from the granite into the gabbro. This
statement holds true for the relations of the gabbro and these
granitic rocks asfar as seen in the region here reported on.
The dikes are not particularly finer grained, either as a whole
or at their edges, than the granite of the main mass, thus in-
dicating the heated condition of the gabbro when the dikes
were intruded. From this and from the relation of these two
rocks in other places it seems likely that the granite, while of
a later date than the gabbro, still is not much younger and
perhaps was intruded before the complete solidification of the
basic rock.

i a

Vi
LIST OF ROCK SAMPLES COLLECTED IN 1893

BY U.S. GRANT.

CONTENTS.
r Page
Minas HOre Ole AK SUPCIIOM aaivsleci: «vis:ciariwe od creas cd sweet koe eee bene. 79
MAM pon mMOrel, Tange 4uweS be cairsies oeiss ots cle teole ool oo ee.s aed! ocleeae ole 7S
SEC IOMSIOL MICHICAM. .-\.2 rock, Soe eamecle e «Seed alee as Seek deetavsese 80
TO YOUMTUGLY 2 2 ee Sate ae Boas oa RE es PR ee ER eS 81
Townships 64 and 65 north, ranges 2, 3, 4 and 5 west................. 81
Batroad on north side of Gunflint lake . 2.53. 8 ics cise cere sew ace 85
AeA ROWE! (5.0 uals s wes chere Een la trae ree ae Aue ae IE Hanes ake te hears 86

An opportunity has not been offered for the study of these
rocks since they were collected; consequently the names are to
be regarded only as approximately correct. This list is a con-
tinuation of that ending on page 67 of the twenty-first annual
report. The specimens in this series are numbered in green
and can thus be distinguished from those of any other series of
the survey or museum.

NORTH SHORE OF LAKE SUPERIOR.

894, Dark reddish, blotched amygdaloid. Point in S. W.
S. W. i sec. 33, 63-3 E.

895. Dark olivine diabase (‘‘black trap”). Center of W. 4
W. + sec. 20, 62-4 E., Chicago (or Sickle) bay. Same as 1811
N. H. W.

TOWNSHIP 65 NORTH, RANGE 4 WEST.

896. Fine grained, gray gabbro. S. W.4S. E&. 4 sec. 27, at
the Y of the railroad.

897. White pegmatyte, from veins or dikes in the last.

898. Fine grained, gray gabbro, 2 inches from contact with
slate. N.W.458. E. 4 sec. 27, in railroad cut.

(8)

80 TWENTY-SECOND ANNUAL REPORT

899. Coarse, gray gabbro, 2 feet from contact with slate.

900, Fine grained, micaceous schist (altered slate), 6 inches
from contact with gabbro.

901. More micaceous facies of the last, 6 inches from con-
tact with gabbro.

902. Fine grained diabase from dike in gabbro; the speci-
men shows one edge and about half the width of the dike. S.
E. iN. W. i sec. 27, in railroad cut.

903. Small dikes of diabase, + to 15 inches wide, in green-
stone. N. W.45S. H.4.N. W. 4 sec. 28, in railroad cut.

904. Impure, magnetitic quartzyte with films of hisingerite.
S. W. 4 N. H.4sec. 29, 65-4, shaft 2, akeley lake.

905. Graphitic rock. Same place.

906. Actinolitic rock holding pieces of quartz and a gray
cherty rock. S: W. corner of N. W. 4 N. W. 4 secs 27; from
the ‘‘nickel” pit just S. of the wagon road.

907. Some of this gray cherty rock. Same place.

908. Fine grained, black, carbonaceous rock. Hill in the S.
H.4N. H.4N. E. 4sec. 26, just south of the railroad.

909. Fine grained diabase. N. E. 4S. E. ¢ sec. 24, just
north of the wagon road.

IRON REGIONS OF MICHIGAN.

910. Recomposed jasper of Upper Huronian. Millie mine,
Tron Mountain.

911. Potsdam quartzyte showing quartz enlargements. Iron
Mountain.

912. Lower Hurorian maguetite-actinolite schist. Republic.

918. Lower Huronian quartzyte near base of this formation.
Republic.

914. Quartzose pebble from basal conglomerate of the
Lower Huronian. Republic.

915. Jaspery conglomerate at base of Upper Huronian.
Goodrich mine, near Ispheming.

916. Impure quartzyte at base of Lower Huronian. Near

Ishpheming.
917. Greenstone of the Basement Complex. Near Isphem-
ing.

918. Carbonate rock of Lower Huronian. Neay Ispheming.

919. Volcanic ash of Upper Huroniahn: Near Ironwood.

920. Cherty carbonate of the Upper Huronian. Palm mine,
near Bessemer.

STATE GEOLOGIST. 81

921. Carbonate changing to ore, Upper Huronian. Black
river. east of Bessemer.

922. Granite of Basement complex. Near Bessemer.

923. Recomposed portion of the same forming a conglomer-
ate that rests on the granite.

924. Chert with ‘bands and shots of ore.’ Colby mine,
Bessemer.

DULUTH.

9%5 Very fine grained, black rock. Crossing of Piedmont
and Lake avenues.

926. The same showing irregularly outlined, foreign pieces.

927. Same as the last.

928. The same with yellowish, vein-like forms.

TOWNSHIPS 64 AND 65 NORTH, RANGES Zz, 3, 4, AND 5 WEST.

929. Coarse, vitreous quartzyte. N. E. + N. E. 4 sec.
34, 65-5.

930. Finely laminated magnetite and impure quartzyte. N.
W. iN. W. isec. 35, 65-5.

“931. Coarse diabase (or gabbro) from center of sill. Port-
age in N. 4 N. W. 4 sec. 35, 65-5.

931A. Finer diabase, 4 inches from top of same sill.

932. Diabase from center of dike in gabbro. Just north of
the small island in N. HE. $ S. E.4sec. 84, 65-5, Kakigo (or
Black Trout) lake.

933. Fine grained; gray gabbro. N. H. 4 N. E. 4 see. 12,
64-5, Big Round lake.

933A. The same in contact with coarse gabbro.

934. Biotite granite from dike in gabbro. Near W. quarter
post of sec. 7, 64-4, point in Big Round lake.

935. Fine grained, olivine gabbro. S. H.158S. W. 14sec. 6,
64 4, Big Round lake.

936. Diabase from center of dike, 8 feet wide, in gabbro. S.
H.iS. W. + sec. 8, 64-4, Big Round lake.

936A. Diabase and gabbro in contact. Same place.

9386B. Film of diabase, 4 inch wide, in gabbro. Same place.

937. Gabbro with a green stain. N. W.iS. E. + sec. 9, 64~
4, north shore of Little Copper lake.

938. Fine grained, gray granite. Near west edge of S. W. 4
S. W. 4+ sec. 16, 64-4.

939. Fine grained, olivine gabbro. N. W. corner of S. W. 4
N. W. i sec. 5, 64-4, south shore of small lake.

82 TWENTY SECOND ANNUAL REPORT

940. Slaty greenstone. A few rods south of the west quar-
ter post of sec. 22, 65-4.

941. Gray syenite. West quarter post of sec. 22, 65-4.

941A. Thesame. Same place.

942. Grain syenite and greenstone in contact. N.S. W.¢
sec. 22, 65-4.

943. Magnetite iron ore from a bed 3 feet thick and about
110 feet below the surface. Shaft 1. S. E. + N. E.4sec. 28,
65-4.

944, Quartzyte, below gabbro sill S.W.i5S. EH 4N.H 2
sec. 29, 65-4, within a few rods of Akeley lake.

945. Fine grained gabbro within six inches of bottom of sill.
Same place. |

946. Coarse gabbro from center of sill. Same place.

947. Quartzyte above gabbro sill. Same place.

948. Gabbro. S. W. +N. E. 4 sec. 29, 65-4, the most east-
ern island in Akeley lake.

949. Gabbro from sillin quartzyte. S. H.4N.E. }sec, 28,
65-4, railroad cut.

950. Cherty carbonate. S.} N. W.2¢ N. HE. ¢sec. 24, 65-4.

9504. A rusted phase of the same. :

951. Coarsely porphyritic diabase. S. E.4N. W. see. 19,
65-3, railroad cut just west of the narrows of Gunflint lake.

052. Diabase. Near south side of S. W. iN. W. 4 see. 19,
65-3, railroad cut, north side of Animikie bay, Gunflint lake.

953. Contact of lower edge of diabase sill and slate. Near
north side of N. E.1S.E. i sec. 24, 65-4, railroad cut at head
of Animikie bay, Gunflint lake.

954. Flinty band in slate. Near same place.

955. Diabase. Near same place.

956. Caleareous deposit on. face of cliff. S. W.4 N. E.¢
sec, 24, 65-4, east end of large hill.

957. Conglomeratic portion of the slate. Same place, at foot
of hill.

958. Breccia cemented by green amphibole. Same place,
top of hill.

959. Peculiar markings on surface of slate. Same place,
about half way up the hill.

960. Black; flinty slate. S.W.iS. EH. 4 sec. 24, 65-4, cliff
on south shore of Cross river.

960A. Another phase of these slates. Same place.

961. Black carbonaceous rock, scratched side is on line of
contact between slate and this rock.

STATE GEOLOGIST. 83

961A. Slate, scratched side is on line of same contact.

961B. Black carbonaceous rock, 30 inches above contact.

961C. Same, 15 feet above contact.

962. Black carbonaceous slate. Near center of N. 4 sec. 30,
65-3, south shore of Gunflint lake.

963. Black carbonaceous rock showing peculiar markings.
Top of hill in N. W.iN. E. 4 sec. 25, 65-4.

964. Diabase from dike. N. W.iN. E. + sec. 25, 65-4.

965. Biotite gabbro. Near center of west side of S. W.4
sec. 25, 65-4.

965A. A phaseof the same. Same place.

966. Gabbro. Near center of S. 4 sec. 25, 65-4.

967. Coarse grained diabase. 18 feet above contact with
slate, top of cliff. S. E.}N. E.4sec. 29, 65-3.

967A. Fine grained diabase, 10 inches above contact.

967B. Fine grained diabase, 5 inches above contact.

967C. Fine grained diabase at contact; the side on the con-
tact is scratched.

967D. Slate at contact.

967K. Slate.

967K. Slate. Theupper surface of these specimens of slate
are scratched; these pieces were in contact with each other.

968. Hard siliceous slate. Near east edge of N. E.4S. E }
sec. 25, 65-4, 100 yards S. W. of the road.

969. Slate, 15 feet below contact with gabbro. Near center
of S. EH. 4 sec. 25, 65-4.

969A. Slate, 4 feet below contact.

969B. Slate, 3 feet below contact.

969C. Contact of slate and gabbro.

969D. Gabbro, 1 foot above contact.

969K. Gabbro, 25 feet above contact.

970. Spotted, black, carbonaceous slate. S. E. 48. W.¢
sec. 29, 65-3, north er lower cliff of Prospect mount.

971. Gray, cherty rock from bed 9 inches in thickness.
Same place.

972. Slate spotted with small white crystals. S. E. 45S. W.
+ sec. 29, 65-8, main cliff of Prospect mount.

973. Fine grained black rock with small blotches. Same
place.

974. Black slate, one-half inch from lower surface of diabase
sill. Same place.

974A. More fissile slate, 10 inches below sill.

‘aie yy?
(Aes ?
4 é

84 TWENTY-SECOND ANNUAL REPORT

975. Coarse grained diabase. N. HE. 4N. W. 4 sec. 32, 65-3,
top of Prospect mount.

976. Gabbro? N. HE. 4N. E. } sec. 31, 65-3.

977. Coarse grained porphyritic diabase. Sec. 27, 65-3,
north shore of Loon lake.

977A. Coarse grained diabase, not porphyritic. Same place.

978. Fine grained siliceous slate. S. W. +N. E. 34sec. 382,
65-3, southwest corner of Loon lake.

979. Gabbro. Top of ridge at same place.

980. Fine grained, gray quartzyte. Near center of N. 3 sec.
35, 65-38, north shore of point in Loon lake.

980A. Same, banded with black slate. Same place.

981. Spotted black slate. West line of sec..27, 65-8, a short
distance north of the quarter post.
- 982. Dark siliceous slate, one inch below diabase sill. S. E.
iN. W. 4 sec. 35, 65-8, hill on point in Loon lake.

983. Gabbro. Near center of E. 4 sec. 32, 65-3, near south-
west corner of Loon lake.

983A. Fine grained, biotitic rock. Near same place.

983B. Siliceous slate. Near same place.

984. Fine grained, reddish weathering, gray quartzyte. N.
iN. E.45S.E. + sec. 32, 65-3, near southwest end of Loon lake.

985. Gabbro? A few rods south of the last.

986. Gabbro? West line of sec. 34, 65-8, one-fourth mile
south of Loon lake.

987. Mottled dioryte. N. W.4S. E. 4 sec. 34, 65-8, on road.

988. Gabbro. N. W.1iS. E. 4 sec. 35, 65-8. Between road
and Loon lake.

989. Olivine gabbro interbanded with coarser gabbro. S.
W.iN. W. +sec. 11, 64-3.

989A. Coarser gabbro. Same place.

990. Gabbro. S. W. 1 sec. 11, 64-3, south shore of lake.

991. Gabbro. S. E. iN. E. + sec. 11, 64-2, Poplar lake. se

992. Diabase. N.- E. + N. W. ¢ sec. 34, 65-2, top of hill at
east end of lake Emma. )

992A. Fine grained, porphyritic diabase. North side of
same hill.
' 993. Micaceous schist. N. W. iN. E. 4 sec. 34, 65-2, portage
between No-Name lake and lake Emma.

994. Diabase. West line of sec. 36, 65-2, 500 feet south of fee
No-Name lake.

995. Coarse grained, gray diabase. N. E.45S. E. 14sec. 35,
65-2, north shore of No-Name lake.

STATE GEOLOGIST. 85

996. Fine grained, gray quartzyte, scratched side was one-
quarter inch below diabase sill. Near center of sec. 27, 65-2.

996A. The same, 13 inches below diabase sill.

997. Diabase. N. E. +S. W. 4 sec. 22, 65-2, north shore of
South lake, just west of the International Boundary portage.

997A. A phase of thesame. Same place.

998. Fissile, black, carbonaceous slate. S.W. 4S. E. 4 sec.
21, 65-2, west end of South lake.

999. Fine grained diabase showing effects of weathering.
N. W. iN. W. 4 sec. 25, 65-2, portage leading south from
South lake.

1000. Breccia of black slate. A short distance north of the
S. E. corner of sec. 24, 65-2, south of South lake.

1001. Diabase. W. 4 sec. 22, 65-2, portage between North
and South lakes.

1002. Cherty carbonate with rusty-weathering areas; not in
place. Sec. 21, 65-2, North lake.

1003. Jasper. Near center of N. E. 4 sec. 16, 65-2 south
shore of narrow arm of North lake.

1003A. Jasper with green and red granules. Same place.

1008B. Gray rock with granules, associated with the jasper.

Same place.

1004. Fragments of red jasper, with granules, from the
beach; not in place. South shore of North lake just east of
the portage to South lake.

1005. Green rock with granules. Pits in N. W.18. W. 4
sec. 16, 65-2.

1005A. A more flinty phase of the same.

1005B. A rusted phase of the same.

1005C. Black fiinty rock.

1005D. Finely banded jasper and magnetite.

1005E. Magnetite iron ore.

Railroad on north side of Gunflint lake.

- 1006. Flint. A short distance west of the rapids between
North and Gunflint lakes. Nos. 1006 to 1007C belong to the
Animikie.

1007. Contact of diabase and flint.

1007A. Gray branded flint.

1007B. Finely banded jasper.

1007C. Cherty carbonate, changing to limonite.

1008. Sheared quartz porphyry. Nos. 1008 to 1008C be-
long to the Keewatin.

86 TWENTY-SECOND ANNUAL REPORT

1008A. The same showing weathered surface.

1008B. The same showing contact with a non-porphyritic
rock.

1008C. Argillyte.

ELY AND TOWER.

1009. Altered diabase. Ely.

1010. Coarse quartzose rock. South of Stuntz bay, Vermil-
ion lake.

1011. Matrix of conglomerate. Just south of western side
of Stuntz bay, Vermilion lake.

1011A. Pebbles from the same.

1012. Sericitic schist with quartz grains. Ely island, Ver-
milion lalxe.

1013. More massive form of the same. Same place.

1014. Augite porphyryte ?, showing one-half the width of a
dike. Same place.

1014. The same, from a point where the dike was 3 feet
wide; center of-dike.

1015. Greenstone. Just south of Tower.

1016. Jasper with fine white veins. Tower.

Py ie ee oe

Wy:

LIST OF ROCK SAMPLES COLLECTED IN 1893*

BY A. D. MEEDS.

These samples were collected in ranges 12 to 15 (inclusive)
west of the Fourth principal meridian, and between lake
Superior and the Vermilion iron range. No examination in
the laboratory has been made of these rocks, so the designa-
tions are only approximately correct. Rocks of this series are
numbered in white, each number followed by the letter M, to
distinguish them from the other series of the survey and
museum. .

1. Medium grained gabbro. E. line of sec. 36, 61-12.

2. Very fine grained gabbro, with black lines. KE. line of
sec. 3, 60-12.

2a. Crystallized quartzyte. Same place.

28 Sameas No.2. Same place.

3. Red, hornblende granite. Center of N. 4 sec. 10, 61-13;
north shore of Stuntz lake.

4. Gray, hornblende granite. Near S. E. corner sec. 15,
61-13; south shore of Stuntz lake.

4a. Phase of the same. Same place.

4b. Granite. Same place.

4c. Pinkish granite. Same place.

4d. Very fine grained, gray granite. Same place.

0. Rather fine grained, olivine gabbro. W. line of sec. 25,
61-12, near quarter post.

6. Fine grained, olivine gabbro. N. E. 4S. W. 4 sec. 10,

60-12; end of portage on Dunka river.

*This list was prepared from Mr. Meeds’ specimens and note books by Dr. U. S. Grant.

88 TWENTY-SECOND ANNUAL REPORT

7. Fine grained, magnetic quartzyte. W. line of sec. 17,

60-12.

7a. The same showing pitted, weathered surface. Same
place.

8. Mica schist. S. HE. 458. E. $ sec. 35, 60-13.

9. Coarse grained gabbro. N. W. 4N. W. 1} sec. 6, 59-12.

10. Magnetic iron ore. W. side of N. W.4N. W. 4 sec. 14,
59-14.

11. Phase of the same. Same place.

12. Hard hematite. N. EK. 4sec. 11, 59-14; Mallmann mine.

13. Hard hematite. Sec. 18, 59-14; Stone shaft.

14. Impure hematite. Near same place.

15. Quartzyte. Aurora pit; probably in S. E. } N. HZ
sec. 24, 59-15. (Missing). -
16. Fine grained quartzyte. Near N. line of sec 24, 59 15.

17. Pinkish gabbro from boulder. Sec. 24, 58-12; island in
Seven Beaver lake.

18. Gabbro. S. W.4S. E. }$sec. 31, 54-13.

18a. The same with magnetite. Same place. |

19. Olivine gabbro. N. W.4N. W. 4 sec. 15, 54-13; end of
portage on Cloquet river.:

19a. Phase of the same with much olivine. Same place.

19b. Phase of the same. Same place.

19c. Rough-weathering phase of the same. Same place.

20. Olivine gabbro. Near north edge of N. W.4sec. 15,
54-13; middle of portage along Cloquet river.

21. Fine grained, micaceous quartzyte. Sec. 18, 59-14;
Stone mine.

23. Jaspery conglomerate. Same place.

23. Micaceous slate. Same place.

24. Limonitic shale. Same place, top of shaft.

25. Magnetic taconyte. Below last.

26. Dark, slaty taconyte. Same place.

27. Jasper. Bottom of shaft.

27a. Purplish taconyte. Buttom of shaft.

28. Siliceous shale. N. EH. of shaft.

29. Hornblende granite. Near Hinsdale.

30. Fine grained diabase from dike. N.edge of N. EH. $
N. E. 4 sec. 24, 55-12.

30a. Quartzless porphyry. Same place.

31. Gabbro near dike. Same place.

32. Reddish, mottled dioryte. Same place.

33. Contact of diabase and gabbro. Same place.

+ PS ae

STATE GEOLOGIST. 89

34. Mottled dioryte from another dike. E. edge of N. E. }
S. E. 4 sec. 24, 55-12.

35. Olivine gabbro from boulder. N. W. 4sec. 24, 55-12.

36. Fine grained, red syenite. W. line of sec. 23, 53-12; in
creek bed.

37. Fine grained, red syenite. S. line of sec. 36, 53-12.

37a. Phase of the same. Same place.

38. Fine grained, red syenite, not in place. Near Highland.

39. Dioryte. N. W.4N. W.4 sec. 34, 53-12.

40. Coarse grained, olivine gabbro. N. line of sec. 5, 54-13.

41. Coarse grained gabbro from boulder. A little west of
the last.

42. Coarse grained gabbro. N. E.4N. E. }sec. 30, 53-14;
southeast shore of Boulder lake.

43. Coarse grained gabbro with long, slender feldspar crys-
tals. N. E. + sec. 18, 53-13; falls in Cloquet river.

44. Anorthosyte from boulder. S. E. 4S. EH. } sec, 19, 53-138;
dam in Cloquet river.

44a. Phase of the same with darker areas. Same place.

45. Coarse grained gabbro. N. EH. 41sec. 36, 53-14; rapids
in Cloquet river.

46. Olivine gabbro. S. E. 1sec. 35, 53-14; falls in Cloquet
river.

Vai,

PRELIMINARY REPORT OF A RECONNOISSANCE
IN NORTHWESTERN MINNESOTA DURING
1895.

BY J... "2ORE:

ITINERARY.

Having been met by my assistant, Mr. H. B. Hovland, at
Minneapolis, we left that city June 22d for Thief River Falls.
At that place I engaged Mr. J. C. O’Brien, an experienced
‘‘cruiser,” to accompany us on a trip on foot through the
northern parts of the Red Lake Indian Reservation, completed
my outfit, and engaged an experienced hunter to take us with
his team to an old hunting camp about thirty miles northeast
of Thief River Falls. My purpose was to keep a northeast

course, if possible, till we struck the survey of the Duluth and _

Winnipeg railroad, and then to explore the so-called ‘‘Beltrami
island of lake Agassiz.”’*

We left Thief River Falls June 26th, and Cook's shanties in
N. W. + of see. 19, T. 156, R. 89 (the before mentioned hunter’s
camp) on the morning of the 28th. We kept a northeast course
as nearly as was practicable in trackless swamps and for many
miles through wind-falls where we did well if we advanced five
miles a day. Besides, we lost some time on account of rain.
Failing to find the railroad survey, probably because its trace
was obliterated by fire, we kept our course till we struck the
Rainy river about five miles above its mouth, July 12th. Hav-
ing there built a raft, we descended the stream till we found
settlers. At Hungry Hall we bought a new birch canoe and
proceeded to the Lake of the Woods and along its southern
shore to Long point. Thence we retraced our course, going

*Warren Upham, in American Geologist, vol. xi, pp. 423-425, June, 1893.

STATE GEOLOGIST: 91

up the Rainy river to Pinewoods P. O., where we took the
steamer ‘‘Shamrock” to the mouth of the Big fork, proposing
to ascend it and the Sturgeon river,* its main western branch,
to a portage into the Tamarack river, which we should descend
and then cross Red lake to the Red Lake Agency. Owing to
misinformation. we ascended the wrong one of the numerous
branches of the Sturgeon river, and somewhat rashly aband-
oned our canoe not far from the northwest corner of T. 154, R.
27. Taking our packs, we traveled southwest and west to the
south branch of Tamarack river, made a raft but found the
stream closed by the work of beavers, and then, striking a
recent land survey near the southwest corner of sec. 24, T. 154,
R. 29, we followed it due west from there to Red lake a little
south of the mouth of the Tamarack river. We arrived at the
Indian village at ‘‘the Narrows” the morning of August 3d,
hired a canoe, and reached Red Lake Agency late August 4th.
Here Mr. O’Brien left us, we bought another canoe, and hired
au Indian to take us and our outfit in a wagon to the head of
Turtle lake, the spot which Beltrami considered the hydro-
graphical center of the continent. We were landed at this
point about noon, August 8th.

We proceeded down Turtle river (making two long portages
above Turtle River lake) to Cass lake, and thence went up the
Mississippi to lake Bemidji, arriving the 16th. Thence we
went south up the Schoolcraft river to sec. 3, T. 144, R. 34,
where I obtained a fine view of a wide region from the top of a
high spruce, and then returned to Bemidji. There we left our
canoe and engaged passage with a settler going by Bagley’s
dam and How’s to Fosston, where we took the cars on the 22d,
Mr. Hovland for Minneapolis, and I for Park Rapids, via Sauk
Center.

From Park Rapids I took a trip along the new railroad grade
to Akeley and on northeast and north into the moraine north
of Eleventh lake (the head of the Crow Wing river), to sec. 10,
T. 142, R. 32. From Park Rapids I returned to Sauk Center,
then took a flying trip up to Northcote, availing myself of the
courtesy of the Great Northern railway company to see the
country in western Marshall and Kittson counties. I arrived
at Minneapolis August 29th.

I met many intelligent woodsmen and Indians at various
times who gave me numerous valuable facts regarding the re-

*Called Opimabonowin river by Horace V. Winchell, Sixteenth Annual Report,
p. 431.

~ . Fete " Uk ane

92 TWENTY-SECOND ANNUAL REPORT

gion I have been studying, thus supplementing to no incon-
siderable degree our personal observations.

SUMMARY OF PRINCIPAL RESULTS.

The more important results of our summer’s work may be
enumerated as follows:

1. The whole area traversed till we reached Red lake was
shaped by lacustrine action. Though I had confidently ex-
pected to find areas untouched by it, and having the common
glacial topography, I visited none which did not show, wherever
above the marsh, sandy ridges which were evidently beaches.
The highest point found was an abrupt ridge rising about 40
feet above the swamp surrounding it. I have little doubt that
it was crossed by the Duluth and Winnipeg railroad survey be-
fore spoken of. It was about in line with it and almost the only
area which was completely burned off, and that quite recently. 4
The ridge was quite bouldery, about a mile long, trending
northeastward, and seemed to have been a bar detached from
land. We saw higher land a few miles west, but there was a
wet swamp between and we at that time hoped to find the rail-
road survey farther on and follow it. I judge that much of the
region traversed between Cook’s shanties and the Rainy river
was considerably higher than those points, because old beaver
dams abounded at both ends of that trip. Much of the country
between those points was tamarack,spruce, and cedar swamps;
but toward Rainy river, especially, low sand ridges 1 to 5 feet
high abounded. Among these ridges it was noticed that the
swamps were wetter adjoining the south side of each ridge,
which was accounted for by supposing a gentle descent toward
the north. The only stream crossed, which was at a distance
of about fifteen miles southwest of the Rainy river, had a width
of about twelve feet and a depth of two feet, with a strong
current southeastward. It is probably a branch of the Rapid
river.

In our course to Rainy river, we found the marsh, though al-
most continuous, yet not very deep, except about Mud lake,
which is in Ts. 156, Rs. 41 and 42, where there are extensive
grassy quagmires,and south of a small lake said to be the head
of the east branch of Roseau river in or near the southwest
corner of T. 159, R. 33, where a ‘‘muskeg” covers several
square miles. Elsewhere there seemed to be firm sand 2 to 4
feet below the surface of the moss. We tested it at several

ie)

STATE GEOLOGIST. . 9

points. Large boulders not infrequently rose above the moss,
even in open swamps. On our returnfrom Rainy river, we did
not have the opportunity, while in the canoe, of noting the
country; but from examination at several points, and by the
trees and the frequent rills trickling into the streams, we
judged that the same shallow sphagnum swamp prevailed.
Along the lower course of the Tamarack river, east of the north
part of Red lake, we found alder swamps which presented more
serious hindrance, with deep muddy bog holes. These were
probably connected with the work of beavers.

We found prairie covering most of the region from Thief
River Falls to Cook’s shanties, and in patches to the northeast
corner of T. 156, R. 38, also a considerable area 10 or 12 miles
from Rainy river, where a swamp had been burned out and
prairie grass had become the main covering, with here and
there willow patches around the nearly consumed remains of
cedars. The soil was rich, the ground mostly firm, the subsoil
a bouldery clay. This suggests that most of this'region may
be similarly reclaimed. No very large patches of white or red
pine were observed. |

2. Of the higher region, named by Mr. Upham ‘Beltrami
island,” we learned some facts from different hunters. We at-
tempted to sift their stories. The higher portion of it is said
to lie between the head of the War Road river and the Nast
Roseau, I judge not far east of the southeast corner of Kittson
county. The ridges are higher toward the south and rise ‘20
feet or more above the swamps between.” They trend N. E.-
S. W. and are covered with pines. One ridge is five miles wide.
No lakes were noticed except in a big swamp eight or nine
miles long and two miles broad, north of the higher ridges.
The railroad survey runs across this swamp on a strip which
bears tamarack.

3. From Red lake southeast, the country rises quite rapidly
to the level of a plateau which lies on the divide between the
Red lake region and the Mississippi. It is estimated to be, in
its highest portions, about 800 feet above Red lake. it is largely
covered with clayey poplar flats, with groves of pine and hard
maples interspersed. It abounds in lakes and has few eleva.
tions except in connection with the moraines hereafter to be
enumerated. The watershed is not clearly defined. Former
glacial stream channels cross it in several places.

4. Several moraines were crossed in our course.

94 TWENTY-SECOND ANNUAL REPORT

(a). That which divides the two portions of Red lake. We
have no important notes to add to those already published. We
hoped to find trace of its extension to the west, but failed to
discover anything decisive. Probably the higher portion of
‘‘Beltrami island” and the ridge between Jadis and the War
Road river are to be correlated with it, the intermediate por-
tions of this moraine having been levelled by the waters of lake
Agassiz as they were dropped from the ice-sheet or at a later
stage. We were unable also to establish the extension of
this ridge much to the east of Red lake.

(b). Between Red Lake Agency and Cass lake we crossed
four well defined moraines, with a less prominent one between
the two pairs in which the four might easily be grouped. . The
first, counting from the north, we crossed two to four miles
from Red Lake. It lay along the upper part of a rather abrupt
rise from the level of the Agency. Its higher portion rose
about 150 feet above the lake. It presented in fine form the
usual basins and knobs, but the latter were of more even hight
than common and corresponded approximately with the level
of the plain just south. This corresponds, without much
doubt, to the moraine noted last year north of Clearwater lake,
running east across Sandy river, and perhaps to one east of
Fosston, trending south.*

(c). After crossing a quite level clayey strip, we came to
the second moraine, marking another slope and presenting
similar features to the last, about eight miles from the lake
and reaching up to 225 or 250 feet above it. This corresponds
to the moraine crossed last year south of Clearwater lake, and
this year east of Popple, or about ‘‘15 miles east of Fosston.”
There it is trending south.

(d). About two miles north of the northwest corner of T.
148, R. 33, we crossed low ridges rising 10 to 20 feet above the
surrounding clayey plain, as though nearly submerged in it.
They trended north of east. Scattering ones a little farther
north were also noticed. These seem to correlate with a
strip near the Buzzle lakes, crossed east of Bagley dam,
which is on sec. 31, T. 148, R. 35, perhaps also corresponding
to hills west of Spain’s and to some east of Upper Rice lake,
which is on the west side of T. 145, R. 36.

(e). Another well developed moraine was found running
east and west along the north line of Ts. 147, Rs, 32 and 33,
south of Turtle River lake and Turtle lakes. Some hills rose

*Twenty-first Annual Report, pp. 72, 73.

ae
£5

iy CP es

STATE GEOLOGIST. 95

60 feet or so above the lakes. This corresponds to the mo-
rainic belt crossed last year, and again this year, in the north
part of T. 147, R 35. It curves southwest and south, crossing
Grant creek near the southwest corner of the same township,
and running southwest of the Schoolcraft river into Hubbard
county. Some of its inner knobs lie along the west side of
lake Marquette and rise 75feetabove it. It has a still higher
ridge southwest of lake Plantagenet. It seems, according to
reports of woodmen, to correlate with a strip passing Elbow
lake, east of Park Rapids, and said to continue on southeast to
Pillager.

(7). Another well developed moraine was crossed north of
the lake next north of Cass lake; i. e. on the southeast corner
of T. 147, R. 31; also, where the Mississippi flows southward
east of Jake Bemidji. Thence it curves more south, passing
east of Schoolcraft river, and between lakes Sheridan and
Kabekona, thence southeast, south of the latter, and on east-
ward south of Leech lake, where, as I reported last year, I
believe that it forms a re-entrant angle and then runs south-
ward west of Pine lake and on to the western one of the
morainic strips south of Gull lake.

These correlations are of course provisional. The concep-
tion which, was suggested last year seems to be corroborated by
the observations of this. Its main features are that two lobes
of the ice-sheet, one occupying the Red lake region, the other
the basin of lake Superior, were at first confluent, but after-
ward becoming reduced first deposited the moraine (d); that,
later, the former of these ice lobes accumulated the moraine (c)
on its south margin, and the other (e) on its northwestern
margin. Still later they similarly formed, respectively, (b)
and (f), each contemporaneous pair of moraines being farther
apart toward the southwest and probably forming a sharp re-
entrant angle or interlobate moraine toward the northeast.

5. Exposures of bed-rock are comparatively rare. Those
observed may be enumerated as follows:

(a). On the south shore of the Lake of the Woods three
granite points run out into the lake. The first on the west,
named Rocky point, was visited last year. The second and longest
is called Long point, the west side of which trends N. 20° W.
(mag.) and consists mostly of gneiss which dips sharply to the
northeast. The rock rises about 20 feet above the lake. Stony
point, a short point about a mile east of the last, is faced with

96 TWENTY-SECOND ANNUAL KEPORT

gneiss for several rods, and is said to have, about a quarter of
a mile from the shore, a rocky knob rising some 50 feet above
the surrounding country. We did not explore it on account of
rain. Several rocky islets appear off these points.

(b). At Zipple’s fishery, near the mouth of Sand creek, is a
low knob of dark magnetic ‘‘gabbro”, and about half a mile
west is an extensive mound of a similar rock rising 40 feet
above the lake. These rocks were all evidently shaped by land
ice, though glacial striz were not common. The few noted were
east of south.

(c). No other outcrops were found till we reached Rapid
river. A few rods above its junction with Rainy river, it falls
over a high ledge of black siliceous schist or slate. The rock
rises about 30 feet above the Rainy river, and the falls are per-
haps 20 feet high. A ledge of magnetic ‘‘gabbro” with granite
juts out on the American side at water level about a half mile
east of Rapid river. !

Having glanced over Dr. Lawson’s report on the Rainy river
region to the Canadian government, and Mr. H. V. Winchell’s
account in the Sixteenth Annual Report of the Minn. Geol.
Survey, I forbear saying anything further about other rock ex-
posures on the Rainy river and the Big fork,

No ledges of Paleozoic rocks were found. In the: bed of a
rapid near the center of sec. 28, T. 148. R. 32, on Turtle river
just above Turtle River lake, I found the bottom of the stream
covered over several square yards with limestone pebbles and
calcareous mud, but found no rock in position. Mr. Joseph
Sombs of Park Rapids, who has spent some time ‘‘cruising”
and also on a claim in T. 150, R. 31, says that on the south side
of Black Duck lake there is much limestone along the stream
for six or seven miles, that the masses of stone are not worn,
and that the south bank is ‘‘50 to 60 feet high.”’

Black Duck river is represented by several from that region
as the main stream running into Red lake. Mr. O’Brien states
that, when Red lake first freezes in the fall, there is left a nar-
row strip of open water reaching from the mouth of Black
Duck river across the south part of the lake to the outlet, Red
Lake river. which remains open considerably longer than the
rest. Iregret that time did not allow me to ascend the east
branch of ‘l'urtle river and go over to the head of Black Duck
river and examine what is spoken of as one of the most pro-
mising tracts for agriculture in that part of the state.

VILL.

NOTES ON THE GEOLOGY OF ITASCA COUNTY,
MINNESOTA.

BY G. E. CULVER.

CONTENTS.

Page
a PC ONT a enh Soro elena a i ciclaio are sine eo eras. soe hte lave alk Sea eels 97
PAOD RIN Y Eaves oad «cael os Nargiapableyaisle » eloje eae Senet ch Mra, cones SP RTE 98
peace Siam AUS WiaMlpoSiestersette ie) ei spares os, otce a aS reviers eee otc becoohtes 100
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INTRODUCTION.

The field season of 1893 was spent by the writer in an exam-
ination of portions of Itasca county. Mr. H. C. Carel of the
University of Minnesota acted as topographer.

The plan of the work included a somewhat careful survey of
two special areas which had been selected by the State Geolo-
gist for more detailed study, together with as thorough a re.
connoissance of the remainder of the county as circumstances
would permit. Particular attention was to be given to the

98 TWENTY-SECOND ANNUAL REPORT

region between the Big fork and the Little fori of Rainy river.

The special areas covered the part of the Mesabi range
lying in Itasca county, and included about three hundred
square miles. The topography was indicated by fifty foot con-
tour lines drawn on the township plats.

When the work on these areas was completed, the region
lying immediately north was examined. The lineof travel was
through Wabano, Trout, Spider and Ruby lakes to the water-
shed between the Mississippi river and Hudson bay, which was
crossed in T. 59-25. The region about the headwaters of
Prairie river was inaccessible on account of the obstruction
of Prairie river by logs. Accordingly the trip down the Big
fork or Bowstring river was next undertaken. It was ex-
pected that the return trip would be made by the Little fork,
but the water was found to be so low that this route had to be
abandoned and the home trip made by way of Rainy lake,

Black bay, Kabetogama and Namekan lakes, and the Vermilion
river.

The weather was exceedingly favorable for field work during
the summer. The low stage of water in the rivers was a hind-
rance to travel, compensated for somewhat by the better expos-
ure of some rock outcrops.

The whole county is so deeply drift-covered, in all but the
northeast portion, that rock exposures are few and far between.
Days and weeks of tramping through the dense brush in
search of outcrops were rewarded only rarely by finding them.

The Big fork and Little fork had been traversed in 1887
by Mr. H. V. Winchell, and although he made a very rapid
journey, he gathered a great amount of information aud made
many valuable observations, besides collecting a number of
rock specimens. His notes* were of much advantage to me.

TOFOGRAPHY.

In all the southern and central parts of the county, so far
as I saw it, the topographic features are very largely due to
the action of the great ice-sheet.

Before the advent of the ice the region was probably a level
one, comparatively speaking. There were here and there
ridges, which still remain; there were also valleys, which
may have been deeper than the present ones, as the hills were,
no doubt, higher, so that a somewhat stronger relief prevailed
then than now.

*Geol. and Nat. Hist. Survey of Minn., 16th Ann. Rept., for 1887, pp. 395-478, with map.

STATE GEOLOGIST. 99

That the ice covered the region for a very long time is a
necessary result of its great southward extension. Neverthe-
less it seems to have changed the topography rather more by
filling than by local erosion. Of this the thick mantle of drift
is evidence. The character of the rocks may account for this
fact, but the ridges of soft Cretaceous rocks seem also to have
withstood the action of the ice.

On its retreat the ice seems to have given up its occupancy
with considerable reluctance. The disposition of morainic ac-
cumulations indicates many halts in the final retreat.

In the immediate valley of the Mississippi a considerable belt
of stratified drift occurs. It forms irregular terraces, which
are rarely true river terraces, beingsand plains formed by the
wash from adjacent moraines. The belt of this material varies
from one to five or more miles in width. In the wide places
the plains often slope steadily down to swamps.

Plains of a similar character are found in the valley of
Prairie river and its tributaries. A good example is found in
the region of Wabano and Trout lakes. The east half of T.
57-25 and the east two-thirds of T. 58-25 are occupied by a prac-
tically continuous plain, separated by the lakes named from a
moraine running roughly parallel with the plain. In both these
townships, but particularly in T. 58-25, numerous lakes are
sunk deep below the level of the plain. These lie nearly at the
same level, so that while the surface of the plain rises to the
north the water level in the lakes is maintained and their sur-
faces are found to be steadily farther below the surface of the
plain as we gonorth. In the southern part of the plain they
are from forty to fifty feet below the plain, and in the northern
part eighty to ninety feet below. Many of them have no out-
lets.

The large lakes, Trout and Wabano, as well as half a dozen
smaller ones, form a chain extending from the water shed in
T. 59-25 to Prairie river. This chain of lakes marks the posi-
tion of an old drainage line or valley in the expansions of
which the lakes now lie. The plain just noted lies immediately
to the east and rises from fifty to ninety feet above the water.
A moraine lies close along the west side of the valley.

It will be seen that the water in the chain of lakes lies very
nearly at the same level as that of the lakes which are sunk in
the plain.

The valley is narrow and somewhat gorge like between Trout
and Ruby lakes in T. 58-25, a distance of amile andahalf. Its

ot AO awed At

100 TWENTY-SECOND ANNUAL REPORT

width in this portion is a quarter of a mile and it is ninety feet
deep. The eastern side is steep.
In all the rest of the upper part of the valley it appears to
be mature. Clearwater creek, which connects Wabano lake
with Prairie river, is a postglacial stream. The old valley
was filled by the stratified drift below Wabano lake.

I.—LAKES AND SWAMPS.

Knobs and kettles are abundant in this part of the county.
The depressions are sometimes dry ‘‘kettles,” but more often
by far they are either swamps or lakes, both of which are
almost innumerable and of sizes varying from a few rods
across up to lakes several miles in diameter and swamps which
cover a township.

IIl.—PREGLACIAL RIDGES (CRETACEOUS).

Rising above the morainic accumulations in some places are
various hills and ridges, some flat-topped, more oval, and
others narrow and elongated. The morainic hills are almost al-
wayssandy. These hills are alwaysclayey. Very few boulders
are seen and the coat of blue clay tillis very thin. The timber
on these ridges is nearly always maple, while that on the
other hills consists of birch and other soft wood.

The largest of these ridges is found in the southern part of
T. 54-26, southwest of Pokegama. lake. It is a long and - ;
rather narrow ridge with northeast by east trend and rises
three hundred feet above Pokegama lake. Its north flank is
covered by heavy morainic accumulations, which do not how-
ever reach its summit. They abound in kettles and irregular
depressions often seventy-five feet and sometimes more than
one hundred feet in depth.

Another hill oval in shape rises one hundred and-fifty feet
above Pokegama lake in sections 22 and 23, T. 55-26. Itis
like the ridge just noted in all but shape and elevation and
like it is flanked on its nurth side by a moraine.¢

From the fact that these hills, of which these two are types,
are apparently of blue clay at the surface,and from the further
fact that in shallow cuts, made in grading logging roads, I
found what I think was Cretaceous shale in small fragments
only, I am of opinion that they will prove t> be Cretaceous
outliers which have withstood the gnawing of the streams and
the grinding of the ice and yet endure to mark the former
eastward extension of the great Cretaceous sea.

STATE GEOLOGIST. 101

Viewing the topography of the district as a whole, it is seen
to be almost entirely recent in origin. Drainage is not yet
fully established. There has been very little postglacial
erosion. The precipitated moisture collects in the numberless
swamps and lakes and there remains. The supply is only a
little more than the demands of evaporation and the needs of
the abundant vegetation. The large lakes have outlets, but
they constitute the exception.

The northern part of the county is apparently quite level,
especially towards the west. However, less was seen of this
portion and it may be that there are topographic features here
not now known, which will appear when the timber is cleared
away.

It is not improbable that the suggestion made by Mr. H. V.
Winchell, that this region lies in that covered by lake Agassiz,
will prove to be correct. Still no important evidence pro or
con, was collected by the writer. Careful watch was kept for
indications of old shore lines and beaches, but none were seen.
Sections along the river did not show beds which could be at-
tributed to ary but river or ice action. Through T. 61-25 and
T. 62-25 moraines were noted crossing the river. Beds of
sand washed down from these moraines are common, but else-
where only clay was seen along this stream (Big fork). The
banks of the Little fork are of the same nature, so far as they
were seen by me.

IIl.—ROCK BASIN DISTRICT.

The topography of the northeastern part of the county is,
in 1nany respects, quite different and constitutes a distinct dis-
trict. Going up Rainy river, we pass, at the Koochiching falls,
somewhat abruptly from a region so deeply drift-covered that
rock is seen only in the beds of the streams, to one in which drift
is seen only in depressions in the uneven rock surface or along
the beaches of the lakes. Rock bosses, ridges and knobs are
everywhere, but they seldom rise more than twenty or thirty
feet above the lakes, until the region about the mouth of the
Vermilion is reached. There the rock masses rise to perhaps
one hundred and fifty feet in some cases. Till is scarce until
after the mouth of the Pelican is passed, going up Vermilion
river; at that point the drift begins to thicken again.

The county is thus seen to be separated into three well marked
topographical districts. Roughly speaking, the south two-
thirds of the county constitute the first district. Its topography

102 TWENTY-SECOND ANNUAL REPORT

is mainly morainic. The west two-thirds of the remainder of
the county is an alluvial or lacustrine plain, while the north:
east corner belongs in the district of bare rocky basins and
rocky prominences.

ROCK SYSTEMS OBSERVED.
I. POKEGAMA QUARTZYTE (PEWABIC).

The first rock examined was the quartzyte at Pokegama falls,
on the Mississippi.

This rock appears at intervals along an irregular line extend-
ing from the north end of Pokegama lake, in the S. W. 4 of the
N. E. + of sec. 23, northeasterly to the rapids of Prairie river.
Test pits show the continuation of this rock as far east as the
east line of T. 56-24, where it passes out of my district. Itis
not known to outcrop east of Prairie river, and is only seen in
a few places between the rapids of that stream and Pokegama
falls.

It is a flat lying rock with a low southerly and southeasterly
dip, and seems to have been bowed up into a series of low flat
arches. This feature is more noticeable in the large exposures
near Prairie river.

At all exposures the rock appears pinkish, is rather fine
grained and very hard. At Pokegama falls, where it has been
quarried to some extent, the rock is seen to have been origi-
nally greenish in color. The reddish coloration is due to
causes external to the rock itself. The coloration has penetrated
from the surface and from all fissures and joints toward the
center of the cubical blocks into which the joint-planes divide
it. In some cases the blocks are small enough so that the
change from green to red is complete; in others a greenish core
is surrounded by a pinkish shell, which varies from one to four
inches in thickness. Cross sections of these blocks (figure 1)
show that the change proceeded from all sides.

Fic. 1—Sectious of quartzyte blocks, showing mode of changein color; outside pink-
ish, greenish within. Pokegama falls. 7

STATE GEOLOGIST. 103

Some of the more massive beds toward the base of the section
are very little changed in color. This is well seen in the bed
of the Prairie river, a little above the bridge in the S. E. 4
of sec. 34, T. 56-25, and also at the quarry above Pokegama
falls.

Besides the red coloration, considerable iron ore is found in
the quartzyte at many places, apparently always in the upper
portion of the series. The character of these upper, ore-bear-
ing strata is decidedly different from that of the lower beds.
The ore-bearing rock, when seen in cross section, presents
an irregularly banded appearance; the layers are alternately
sheets of ore and sheets of quartz. As seen under the hand
lens, the quartz layers show no grains; the structure is porous,
and the quartz is usually stained red. The ore sheets vary from
ferruginous quartz to a very good ore. Both ore sheets and
quartz layers are exceedingly irregular and are often inter-
rupted or cut by each other.

ig. 2.—Hand specimen of ore-bearing rock, T. 56-24; showing the irregular band-
ing seen in cross sections. The dotted areas are quartz, the others lean ore.

This irregularity is far greater than any that could have
been produced by the slight movements which have affected the
containing beds, and evidently it dates from the formation of
the ore, whether that was contemporaneous with the formation
of the containing beds or not.

The study of a large number of thin sections of this rock is
necessary to determine the genesis, bcth of the ore and of the
quartz layers.

Whether the ore was deposited at the time of the coloration
of the lower beds, or not, my observations do not determine.
That the latter process was long subsequent to the formation of
the quartzyte is clearly shown by the fact that the coloration
proceeded inward from all joint-planes toward the centers of
the blocks, as already explained. This could not have been the
case if the rock had not already become indurated and jointed

104 TWENTY-SECOND ANNUAL REPORT

before it was bathed in the iron-bearing solution (which seems
to have come from the surface and not from below ).*

It is of course possible that this ferruginous liquid was de-
rived from the ore-bearing portion of the beds at a time long
subsequent to the deposition of the ore. Opportunities for a
thorough examination on this point are notyettobehad. The
test pits are only sunk to the surface of the rock, or a few feet
into it, as the ore, if found at all, is found near or at the sur-
face of the rock.

In places the quartzyte is somewhat conglomeratic. The
pebbles are small, not larger than coarse shot. The conglom-
eratic layers are near the base of the series.

With the exception of the iron ore, this rock very closely re-
sembles the Sioux quartzyte of southeastern South Dakota.

The quartzyte was nowhere seen in contact with any other
rock.

Near the dam at the foot of Prairie lake, just north of the
quartzyte exposure, is a narrow belt on which are thickly
strewn many small boulders of greenish-gray sandstone. No
rock like it is exposed anywhere in this region, at least I was
unable to find any. As represented by the boulders it is a
quartz sandstone, somewhat micaceous, of only moderately firm
texture and inclined to split into flags.

It gives no indication whatever of the presence of iron oxide.
The belt on which the boulders lie is some four or five rods
wide. Passing across this belt toward the quartzyte area, the
sandstone boulders are quite abruptly replaced by boulders of
quartzyte, which occupy a belt perhaps ten or fifteen rods wide,
beyond which the quartzyte in place appears in oval topped
masses here and there, often hidden by the drift but showing
fairly well all the way to the river, a half mile southeast, where
the iron-bearing beds are seen.

It was my impression, while on the ground, that beneath the
belt of quartzyte-boulders the quartzyte lies, and that under
the strip covered with boulders of gray sandstone, beds of that
rock must be (making due allowance for the southward move-
ment, due to ice action).

* With reference to the coloration of the quartzyte it is obvious that there are two
waysin which this might occur. If the greenish quartzyte contains iron in any form
other than the ferric oxide, then simple weathering would produce the change noted.
Nor is there any fact observable in the field that militates against this as the way in
which the change in color occurred. As arule the red coat is as firm as the greencore
Microscopic study would determine this point.

The other way of accounting for the color change is inttiawtell in the body of this
paper.

STATE GEOLOGIST. 105

Just across the river (north) lies a body of granite. Boulders
of this rock are strewn for a short distance to the south of the
granite. Then comes a stretch of swampy ground in which no
boulders can be seen, and after that, the succession before
noted. The relations of these rocks are shown by the section
(figure 3).

Fia. 3.—Showing stratigraphic relations at the falls of Prairie river. 1, granite; 2.
sandstone boulders; 3a, quartzyte boulders; 3, quartzyte in place.

The depression which separates the granite from the near-
lying quartzyte indicates the removal of some easily destroyed
rock,—possibly the gray sandstone, possibly some other rock,
no traces of which were seen,—lying between the tough gran-
ite on the one hand and the hard quartzyte on the other. No
positive evidence, other than that just stated, supports this
view of the stratigraphic relations here announced. On the
other hand, nothing was found which opposes such a view.

II. PRAIRIE RIVER GRANITE.

This rock is exposed in the S. E. 4 of the S. E. 4 of sec. 82
and also in sec. 33, and very abundantly in sec. 34, T. 56, R. 25.
It is seen to lie in a belt parallel to the quartzyte just described.
It is a fine grained gray rock with some gneissic phases, and it
contains some bodies of schist which were taken to indicate
that the granite is eruptive. Its surface is quite uneven and is
marked by roughly parallel ridges or corrugations, which mark
lines of yielding to lateral pressure. These run in the direc-
tion of the outcrop, i. e., northeast and southwest. They are
not high but are noticeable by reason of the incipient folding
or bulging up of the rock.

Thrust planes are numerous and generally have either verti-
cal or very steep dip.

Nothing like bedding was observed in this rock. Its rela-
tion to the quartzyte has already been noticed. The dip of the
latter away from the granite shows that the region has been
slightly uplifted,either by a general movement or by the intru-
sion of the granite. In T. 56-24, in the N. W. + of sec. 9 and
also in the eastern part of sec. 8, outcrops of arock very similar
to the granite rock at Prairie river, occur in the form of low

106 TWENTY-SECOND ANNUAL REPORT

mounds, two in number, a half mile apart. The one in sec. 8
is low-lying and is exposed by the action of a small creek, for
perhaps a quarter of amile. The other outcrop, in sec. 9, is
larger, rising perhaps fifteen feet above the little valley to the
north. No other rock outcrops in this township. Test pits
one mile south of the granite encounter the conglomeratic
phase of the quartzyte, with very little ore. A half mile far-
ther south the ore is found more abundant, and in the central
and eastern parts of the township numerous pits have been
sunk and in each the ore bearing rock was found.

The Diamond mine in the center of the township has been de-
veloped enough to show the presence of a considerable body of
good ore. It was noticed in the sinking of these nits that the
ore and rock were found at very different levels, e.g., one was
sunk in a depression in the top of the highest hill in the town-
ship and another at the foot of the same hill. In the first case
the ore was found at a level about that of the surface of the
ground at the second pit. In the latter the ore was quite as
far below the surface, which shows a difference of level in the
rock surface of 150 feet in an eighth of a mile.

It is noteworthy that among the score of pits in this town-
ship not one seems to have touched the granite.*

Granite was reported in the next township north but it could
not be examined.

Ill. DIORYTES OF THE BIG FORK OR BOWSTRING RIVER.
On the Big fork a few miles above the mouth of Rice river a

ridge of dioryte about fifty yards wide crosses the river running ~

north and south. The river runs at the south end of the ridge
and then makes a bend and cuts squarely across it. The
greater part of ‘the ridge. which rises some twenty feet above
the river. is on the left bank. Its length is less than a quarter
of a mile.

The rock is a rather fine-grained dioryte with possibly some
granitic phases. Quartz and colorless feldspar are the chief
minerals. At the upper end of the exposure some reddish
feldspar was seen.

A small dike of greenstone cuts the dioryte and runs N. W..

by W. Up the river some two hundred yards from the south
end of the dioryte, a low exposure of a dark basic rock, which
looks a little like a gabbro, rises about three feet above the

*The rock here called granite has not been studied by me under the microscope
hence I do not know that the rock is a granite. It may be a dioryte.

STATE GEOLOGIST. 107

water at its very low stage. This may prove to be dioryte also
but is decidedly basic. No contact of it with the dioryte could
be found; nor could any extension of the latter be discovered
in the woods on either bank. Five miles down the river an-
other small body of dioryte, macroscopically indistinguishable
from the exposure just noted, is found crossing the stream and
disappearing in the banks. One hundred and fifty yards
farther down is another mass of the same rock. This rock is
black on the surface, but it may be that this is the result of its
being covered by the stream at high water.

Perhaps five miles farther down the river is another body of
the same rock. It shows in the bed and on the right bank of
the stream. A number of large boulders four to six feet in
diameter, apparently broken from this ledge, lie in the edge of
the river and on the bank close to the solid rock. Their upper
surfaces are striated and the strize are parallel on the separate
boulders and with those on the moutonnéed surfaces of the
ledge.

IV. DIORYTE AT KOOCHICHING FALLS.

The Koochiching falls of the Rainy river are due to a ridge of
quartz mica dioryte which is crossed by the stream about three
miles below the outletof Rainy lake. Tnis rock forms the Amer-
ican shore for a mile below the falls, below which are two good
sized islands of the same rock. It may appear farther down
on the Canadian bank, but does not show itself on the U. S.
side. This ridge of dioryte lies in the midst of a great body of
mica schist* [Coutchiching of Lawson] through which it has
been intruded. As evidence of this, many fragments of the
schist of varying size are to be seen embedded in the dioryte.

Its character is better seen on the two islands than else-
where. On fresh surfaces it appears as a light gray, rather
coarse-grained rock made up of quartz, plagioclose, microcline
and biotite. On weathered surfaces the color is faintly reddish,
and large crystals of feldspar stand up prominently from the
surface, giving a porphyritic appearance to the rock not seen
in the fresh sections. At the upper end of the lower island a
true porphyritic phase of the rock is seen. It changes notably
in color and becomes finer in grain. At the upper end of the
upper island a gneissic phase appears.

*Classed by Dr. A. C. Lawson as a mica syenite gneiss, Report on the Geology of the

Rainy Lake Region, p. 126 F.. (Geol. and Nat. Hist. Survey of Canada, Annual Report,
new series, vol. 111, for 1887-88, Part F.)

108 TWENTY-SECOND ANNUAL REPORT

A greenstone dike cuts the dioryte, passing through the
upper island and then to the American shore, along which it
was traced for a mile, or to the falls, where it crosses the river
and disappears on the Canadian side. Like the dioryte, its
trend is nearly east and west. It varies in width from three to
ten feet. It is probably a diabase.

The dioryte is clearly younger than the schists, and the dia-
base dike is still more recent. Later still slight movements of
these rocks have occurred, which have opened small fissures
on the American shore and produced slight dislocations which
are shown in the schists and also in the diabase dike.

V. THE GREENSTONES.

These appear in two distinct types, which, however, shade or
merge into each other in such a way as to make it often doubt-
ful whether one is dealing with one or the other of the types.
When they appear as dikes, as they often do, they are of course
plainly and purely eruptive. Also they may be and are found
in such condition as to make it certain that we have to do with
beds of consolidated tuffs. But again they are found in such
condition that it is not possible to say to which class they shall
be assigned. Along the Big fork these rocks constitute the
chief exposures between Rice river and Big falls. These ex-
posures are mainly low oval mounds or moutonnéed surfaces
from which the river has removed the drift. No other rock is
found associated with them. In T. 61-25 the greenstone forms
considerable hills, fifty or sixty feet high, and exterding for
several miles. From the foot of Rice River rapids on the Big
fork to Little falls no rock but greenstone is exposed, but the
intervals between exposures are so great there is plenty of
room for other rocks. At the Little falls the river pours over a
large mass of greenstone which here shows nearly all gradations
of that rock. Someof itseems from a microscopic examination
to be eruptive. Other portions appear more like tuffs. No other
rock occurs here. A fracture was noted running across the
exposure.

Two miles down the river a small mound of greenstone is
seen. This is the last noted exceptin the form of dikes. These
will be noticed in describing the beds cut by them. At two ex-
posures, one near the mouth of Deer river and the other a mile
up that stream, pebbles or amygdules of quartz up to two
inches in diameter were noticed in the greenstone. They have
a little elongation which was thought to be due to squeezing.

‘

STATE GEOLOGIST. 109

VI. MICA SCHISTS.

These rocks with the intruded granites, etc., constitute an
immense series, extending, on the Big fork, from a point
about twelve miles by river below the Little falls to within fif-
teen miles of Rainy river. The exposure is by no means a
continuous one for the drift is deep all the way down this
stream, but erosion has uncovered the rock in places enough
to indicate the continuity of the beds. On the Little fork
mica schist was found within four miles of the Rainy river,
while on Rainy lake the rocks are exposed in almost continuous
section. Dr. Lawson* estimates their thickness on Rainy lake
at four and a half miles.

The first exposure of these schists is about twelve miles
below Little falls. The river runs in the schists for about an
eighth of a mile. The rock stands up ten or twelve feet above
the water. Two or three moutonnéed surfaces appear in the
stream rising from one to three feet above very low water.

The rock seems to be composed almost wholiy of biotite and
quartz. The dip and strike were somewhat doubtfully made
out by means partly of quartz lenses which were thought to
indicate the bedding planes, and partly by means of a thin bed
of green rock which was taken to be tuff.

As thus determined, the dip is some 30° or 40° west of north
at an angle of perhaps 85°,and the strike east 30° or 40° north.

The schists are cut by a dike of greenstone, probably diabase,
near the middle of the outcrop. It is twelve feet wide and
strikes south 40° east.

Near the lower end of the exposure, in close proximity to the
supposed tuff bed, an intrusion of granite is seen on the right
bank. It is here twenty feet wide. On the opposite bank
twenty rods away a narrow one foot vein of the same rock is
seen. Itis fine grained, light colored, slightly greenish, and
extremely brittle.

At Big falls is a still larger exposure of mica schist veined
with granite over which the river tumbles in a series of
cascades falling about thirty feet in a quarter of amile. Here
the schists strike 8° or 10° south of east, but with local varia-
tions caused by the intrusion of the granite in the form of
veins, sheets, bosses and dikes.

Two of these granite masses have flexed and Abani the
schists in a very complex fashion. The dip is nearly vertical
except where locally modified by the granite.

*Report on the Geology of the Rainy Lake Region, p. 102 F.

110 TWEN'TY-SECOND ANNUAL REPORT

A dike of greenstone eighty feet wide cuts the schist parallel
with the strike, near the head of the rapids. The schists are
not notably changed at the contact with the dike. The granite
sheets are very numerous. They run parallel with the strike
of the schist and vary in thickness from less than one quarter
of an inch to ten feet. The larger sheets do not follow the
bedding of the schist very closely. They often show gneissic
phases. This exposure extends for two miles along the river,
but could not be found in the woods above the immediate
valley.

A half mile below the mouth of the Sturgeon river—six miles
from Big falls by river—mica schists veined with granite again
appear. Apparently the same rock is seen at intervals in the
river for twenty-five miles, always with a very steep dip to the
north and with strike varying from east and west to southeast-
northwest.

In the bed of Rainy river three miles below the falls a bed of
fine-grained very hard mica schist is seen. It has a dip of 85°
to the north and strikes east and west. Exposures of similar
rock are found to within a mile and a half of the falls. Here it
has been invaded by a large ridge of dioryte which has appar-
ently carried it up so far that weathering and erosion have re-
moved it, exposing the dioryte.

Four miles up the Little fork an exposure of mica schist of
the same hard fine-grained type is seen crossing the river from
northeast to southwest. This is also the direction of the strike.
Dip vertical.

Above Ft. Francis at the Koochiching rapids, along the
route through Rainy lake, Black bay, Kabetogama, Na-
mekan and Sand Points lakes, and far up the Vermillion river,
the schists were seen, sometimes free for long stretches from
any intruded rock, and again seamed in every direction with
granite.

There was usually a gradual increase in the abundance of the
granite until it became the predominant rock, then in passing
along the reverse conditions obtained until the simple schist
was all that was to be seen.

No detailed work was done in this most interesting region,
the time having been consumed in literally ‘‘beating the bush”
in search of outcrops farther southwest in the region so thickly
drift-covered that only rarely was the search rewarded with
anything but negative results.

STATE GEOLOGIST. 111

GLACIAL PHENOMENA.
I. THE TILL.

With some local exceptions, the till of the district is sandy,
often gravelly. There is a notable scarcity of large boulders,
in fact of boulders of any size except in cases to be hereafter
specified.

The drift thins steadily to the northeast, so that by the time
the southeast end of Rainy lake is reached only the depressions
in the rocks are covered by drift.

T. 54-26 is one of the exceptions in that it is nearly all cov-
ered by a blue clayey tili. This is doubtless due to the pres-
ence of the hills referred to on a previous page as possibly
Cretaceous. There is evidence, in the shape of fragments of
shale and pieces of lignite, that considerable areas of Creta-
ceous clays were to be found in this region at the time of the ice
invasion. Blue clay lies under the till in many places in the
southern part of the county. It was also noted along the Mis-
sissippi as underlying the sand and silt on the river bank from
Grand Rapids to the swamp below Blackberry station.

No clayey till was noticed except in the immediate neighbor-
hood of high non-morainic hills and ridges.

II, MORAINES.

A tolerably well-marked and continuous moraine enters this
district in the southwest corner of T. 54-26 and runs northeast
by north through three townships, leaving my territory in the
northeast corner of T. 56-24.

The Mississippi river cuts this moraine two miles west of
Blackberry station in the northwest corner of T. 54-24. At
this point the morainic hills rise one hundred feet above the
river. [A sand plain (overwash plain) lies along the east side
of the moraine in T. 54-24 and the southern part of T. 55-24. |

Four miles north of the river the highest point of the moraine
rises three hundred feet above Trout lake, in sec. 18, T. 55-24.

Somewhat disconnected morainic accumulations extend from
the southern boundary of T. 54-26 north through at least six
townships where they pass into a region not visited.

The frequent interruptions almost invariably transfer the
‘ moraine to the west, so that, while the segments trend about
northeast by north, the moraine as a whole extends nearly due
north.

This moraine has its strongest development in the southern

half of T. 54-26, on the northwest flank of the high ridge of sup-
—8

\ re ee

112 TWENTY-SECOND ANNUAL REPORT

posed Cretaceous beds. It is also well develop :d in the north-
eastern part of T. 56-24.

Along both these moraines knobs and kettles are often well
shown. The latter are in some cases one hundred feet deep.

One peculiar kettle is worth noting. It is in the top of the
highest hill in T. 56-24, in sec. 21. The hill is about one
hundred and fifty feet above the little stream near its base, and
is quite separated from the adjacent hills. The kettle simulates
a crater very closely. It occupies nearly the whole top of the
hill, is about sixty feet deep and fifteen rods across the top of
its narrowrim. The tillis gravelly and quite bouldery. The
boulders are well rounded and some of them well travelled.
This is the only case that has come under my observation, of a
large kettle in the top of an isolated hill.

Ill. BOULDER BEDS.

The scarcity of boulders in the till has already been noted.
In one little area near the granite outcrop in T. 56-24 boulders
were quite plentiful and some were of good size; but in all the
rest of the district the till was found to contain but few boulders.

Whoever makes a canoe journey along either the Big fork
or the Little fork in low water is not likely to complain of the
infrequency of boulders in the bed of the stream. Scattered
boulders here and there, more abundant than in the till, were
to be expected. But that by no means tells the story. At all
too frequent intervals the streams cross thick beds of boulders
which extend in trains for unknown distances. In one case
on the Big fork tae same train was crossed three times in
successive bends of the stream. They often occupy the bed
of the stream for two miles at a stretch, but in such cases it is
probable that the stream crosses the boulder train obliquely.
On the Big fork these beds of boulders were first encountered
alsout ten miles above the mduth of Rice river, and they were
found at intervals all the way to within fifteen miles of Rainy
river. The number of the boulders is astonishingly great.
In some instances the river nearly disappears in the mass of
boulders. More frequently it forms rapids, quite unfavorable
to canoe navigation in low water. At the places where these
boulder beds were found the country was almost invariably
level. Exceptions to this are found in the vicinity of Deer
river. There are no indications of the presence or proximity
of amoraine. There are no signs of a rock outcrop. There
are no boulders on the banks of the stream. They seem to be

STATE GEOLOGIST. Lis

confined to levels not far above that of the water. Whether
these boulder trains mark the position of earlier moraines
from which the other material has been removed, or whether
they are combings from the bottom of the ice-sheet, Iam unable
to say. But from the extension of the belts, and from the fact
that where outcrops occur no such boulder beds are found, and
from the further fact that just above Deer river where a
moraine crosses the stream boulder beds do occur, I incline to
the former view.

IV. GLACIAL STRLA.
The following table gives the results of observations on the

direction of striz, as noted by me, referred to the magnetic
meridian:

ol) UEDUP SE ne 22) Seo ee eae S. 60° E.
PANN EMDVED TATIOS: Goda stc clasts. cs Sussarete e's» oeee Osco 6 Sau S. 4° to 10° E.
Sapnie Tork above Rice river, P.-61-26.. 0. 2 |. cine ecb es cece ee cee E. 15° 8.
On Big fork above Rice river, 40 rods down stream ........ ......0.005, E.
fie fork: below Rice river, TL. 61-26... 52.6 cose. see cence as i hag i la
On Big fork below Rice river, 'T. 61-25. 7...... ..2.0..--00 E. 15° to 45° S.
On Big fork above Deer river, T. 62-25...... ateichatathls.} Mastes E. to BE. 10°S.
Mapbierork above Deer river, i. 62-302... ce ec ve oh sce h es cw lace E. 10°S.
On Big fork at Little falls....... {Ore OSE EHO Onc ale eae ge S. 12° to 18° E.
On Big fork 12 miles below Little falls. .................. E. 10° to 22° §.
a eter EVIS® TALIS ce cholate Scr afslls nia So 015,62) 6 0's aig eesjes aval Sivig ejelad eran ea, oy E.
ieee FORK DelOW SbUISEON TIVET i... le ee eel cces deee cscs S. 34° EF.
Gn big fork 12'miles below Big falls: .. 2.2... .0.6.000 cseees -E 18° to 22° S.
me nipstorkd 2o miles below Big falls... 0... 4 2s .cc ws we, cbc ea os S. 34° W.
On Little fork 4 miles above Rainy river. ..................000. S. 40° W.
On Rainy river 2? miles below Ft. Francis. ..., ccscecc.scecvees S. 30° W.
@n Rainy river 14 miles below Ft. Francis..................... S. 30° W.
Mn wapetorama: lake near Black Day. sci. ve ie. Secc ces ucc ee oeas S. 42° W.
upmramelkan lake: West {CM ), cite 'sjs2-iccselsdieio ooo Baetelc case ce dele en S. 30° W.
On Sand Points lake, 10 miles from Vermilion river.... ........ S127 We
maanwer, SOULR GL Vermilion Take@s.¢. 2.26 ct deci oss es bev wcee cece S. 8° W.

Some interesting facts, relative to the direction of the ice-
movement, are brought out by a study of this table. It is seen
that there is a broad belt in which the movement, as indicated
by the strize, was to the east of south instead of west of south,
as would be expected from previously observed strize along the
north coast of lake Superior and along the lakes on the Inter-
national boundary. The abrupt change from southeast to
southwest, as shown on the Big fork, is certainly suggestive,
in view of the fact that the region is a very level one so that
local topography can hardly be appealed to for an explanation.
Hardly less looked for is the lessening of the westerly move-

114 TWENTY-SECOND ANNUAL REPORT

ment noted in passing from Namekan lake to Vermilion lake,
since the course is directly toward lake Superior. So far as I
am aware, no suggestion of a cause for an easterly movement of
the ice in this region has been made by any one. In fact, I
think it has been generally supposed that the movement to the
southwest along lake Superior and along the lakes of the Inter-
national boundary, as far at least as to the Lake of the Woods,
necessitated a parallel movement in the district lying between
these two. That such was not always the case is shown by
the evidence here recorded.

EX.

PRELIMINARY REPORT ON FIELD WORK DONE

Ill.

IN 1895.

BY J. E. SPURR.

CONTENTS.
Page
PGA ATs Vane rs Bo: reese MES eases ae ote pS, tire aS nthe Whales ncealesatea 116
PANTS AeasEET AU TOTOE Cis ata eree eke ale bstes cota te eee, vacic “ekese Ae ators cueheiesiwis: ale/e'e ayeieieha, Asieis 118
Meme Gr ROUT COM CLOV CL octstee ears: «ere aiiers era's tie wi atbee ciisih a niet steretes es cia adets guar 118
PPR CONGO DIOUNERTOUS 2. txtep ls. sack oc e ak Set ccm wcb¥Ge ude dide aera e 118
Thee Safe) ates aves Coe aah 2 914 2 ee A ee eR Ree ar 118
D2 EI GbE DATES Ole DIC ATCase). wale) Doe seers mks sale cme oes os 118
Se ODOM ECL MeGMOUSiak Maret cats oo: tats a setke vaca yes Boe ciel. sacs s/t eve ale 118
re Pan we MOESAUL TANGO 220 Costs Chins cg cleis clot oe 00% ees 118
Et OPEL MALES Of SLHOIATEA sic 2 nec Hea cies, Hcjourrs a! sle\ecs sieravetotsys 118
SAME. DOMES I DHE PEOLOLV: oh ce ae vcrectecs eg ee eek Ghee eede ohare 119
Pome he Giants Tange erantye: ct ick cow. be elade leo ¥ ec selleds sis 119
Gee GS OSL MOMs ee ct. ee hate ae 2 Sacred ee Pee prods Veale dia de 119
mR ROT Hd Ti eA CA As areca vance S Meteie Since aseunie so Mlsliareithe wraue 119
Ba ane Keewa bila SCTICS 10. <75,6.0 ors!s.das00 cre sors PRIN et fens honie a ate ete 120
Me UCR Dis LANE CISC DISDS 2. crciiuleciine aecluk sane we op 4 sca uoa 120
Ope AL NE? Moreen SCIISESC mie nies ale cease Soe obpoieie Delve Stayefe cremate ts 120
Det Mec OOWbCRIC HIM: PHASE § 125. Serve < 1)o cle divide weve ejenlana 121
Govrne simple Getribal PRASC ss).0.2% a3 Oe ce atas asiee sla ee ce 121
Re CL BOTA LABOR et mete es raids 8 eich aya Lis ag 0/4 oye dos elesate rong 121
a. Some new information as to their extent............. 121
b. Their correlation with other formations.............. 121
eee MUNIN TE BOTIOS so ct. coe east. oe xo sles Skis nd cntla o oa eens She's 122
Breer HACE OUS Ll a2 Susi). cp the brea tta te S00 So Vd Oe OP ne, bap eletel oss 122
Sse MEMEBERS Bsr Lhe ck aiid ne er eMe Sealna fie sJalbracete sierd wovlats Meet a/eiele 122
Re NV OINTE Sf Oe, ions wc IS RES Gc Sl Ps Che ore S aiakesetereiee & 122
PAE LSet MOMS IIS WES ARR. ./2))cSslsilahalte dileacld she e's ee 123

Co EPC ESA SOUP sce ots onic, Yves aolhee wialp 8 elem dine Liebe t's 124

116 TWENTY-SECOND ANNUAL REPORT

ITINERARY.

The writer began his field work at the town of Virginia, in
St. Louis county, where he arrived June 9, 1898. June 23d, he
was joined by a competent assistant, Mr. R. P. Johnston of St.
Paul, who remained with him throughout the rest of the sea-
son. Later in the summer, the change in the methods of
work made it necessary to secure another assistant, and Mr.
N. J. Cavanaugh was engaged at Mountain Iron, and continued
in the employ of the survey from August 14 to November 7.

During the first part of the season it was convenient to make
headquarters at towns and mining camps, along the Mesabi
range, and from there to explore and map the surrounding
country. Soon after my arrival the town of Virginia was de-
stroyed by a forest fire, and during the rest of my stay in the
vicinity, I, with many others, was indebted to the generous
hospitality of Mr. R. B. Green. On June 27 we went to the
mining town of Eveleth, in sec. 31, T. 58-17, where we made
our headquarters; from Eveleth the next move was to McKin-
ley; from McKinley to Biwabik; and from Biwabik to Moun-
tain Iron. Having at length completed the survey of the Me-
sabi in ranges 16-19 west, a reconnoissance of the country to
the north was undertaken. The services of Mr. Cavanaugh
were secured, and on August 15 our party of three left Moun-
tain Iron on foot, with a tent, camping outfit, and two weeks’
provisions in our packsacks. Our route lay along the trail on
the line between ranges 18 and 19, which we followed without
difficulty, save in one case where a detour into T. 60-19 is
made, and where nearly two days were spent in finding it.
This brought us, in the northern part of T. 61-18, to the Stur-
geon river road, which runs west from Tower to Sturgeon
river. This we followed into Tower.

After some slight examination of the vicinity of Tower, two
canoes were bought, and we left the town August 30 and made
our way up the Pike river. The portages upon the upper part
of this stream have been disused for some time, so that pro-
gress was somewhat difficult, and the old portage to the Em-
barras lakes was passed by unnoticed. We therefore kept on
till we reached the county road, afew miles west of Merritt.
From this point a portage was made to the Embarras lake at
Merritt.

In order to gain some idea of the country lying south of the ~
Mesabi range and north of the immediate vicinity of Carlton

STATE GEOLOGIST. ila We¢

county, our party set out again from Merritt September 6th,
and canoed down through the Embarras lakes and Esquagama
lake, through the Embarras river to the St. Louis river and
down this latter stream as far as the crossing of the Duluth,
Missabe and Northern railroad, at Albert. Some attempt was
made to follow this river further down, but passage became
progressively more difficult, on account of log jams, and the
country was so unpromising for discoveries of geological im-
portance that it seemed wise to turn back. At Albert, therefore,
canoes and camp furniture were loaded into a train and carried
to the crossing of the White Face river, at Kelsey. From here
an expedition was made up the White Face river for some
twenty-five miles, and back to the same point. After this trip
the canoes were disposed of, and the rest of the season’s work
was done on foot, with the aid of railroads when these were
convenient. For the reconnoissance of much of the southeast-
ern part of St. Louis county, the Duluth, Missabe and Northern
railroad between the stations Kelsey and Pine (on White Pine
creek) was made a center and base of supplies. On September
28th we packed from Columbia Junction to Stony Brook Junc-
tion, on the Duluth and Winnipeg railroad at the St. Louis
river.

From Stony Brook Junction we worked both east and west,
_ using the railroad, as before, for our base of supplies. On the
west. we worked past Floodwood; and on the east, down into
Carlton county. On October 24th we crossed the St. Louis river
at Nagonab on a log jam, and made our way north along White
Pine creek to the Duluth, Missabe and. Northern railroad.
Crossing this, we kept on northward to the Cloquet river road,
which runs westward from Duluth. Having from this route
completed the reconnoissance of the southeastern corner of St#
Louis county, the same road was followed westward, across the
Cloquet and St. Louis rivers, to Floodwood; and thence north
to Floodwood lake. From Floodwood lake north the trail could
not be followed, but by pressing onward through the woods we
reached the unfinished Duluth, Mississippi River and Northern
railroad, and in a few days arrived at Hibbing, on the Mesabi
range.

At Hibbing, Mr. Cavanaugh left us. From this point and
from the various mining camps in the vicinity that part of the
Mesabi range which lies in ranges 20 and 21 was carefully ex-
amined, so far as circumstances would allow, as far west as the
Mesabi Chief mine in sec. 22, T. 57-22, When this task was

118 TWENTY-SECOND ANNUAL REPORT

completed, the weather had become unfavorable for further
work. We therefore left the field, and on November 18th Mr.
Juhnston and myself reached Minneapolis.

AREA MAPPED.

During the season sixty-two towns were roughly mapped,
both geologically and to some extent topographically. When
it is considered that these represent 2,232 square miles, and
that all the information which we have in regard to them was
obtained by one person in five months, and was secured in
often unfavorable circumstances, it will be seen that there can
be no possibility of having done careful and detailed work on
most of the area, and the errors which will doubtless be de-
tected may be fully accounted for.

GEOLOGICAL METHODS.

Somewhat careful and detailed work was done along the
Mesabi range, in ranges 16 to.21. This is the most varied and
interesting district in the territory examined, both geologically
and topographically. Here the limits and relations of the dif-
ferent formations were carefully traced, most of the test-pits
were visited, and a collection which was especially rich in the
various phases of the iron-bearing rock was made. The open-
ing up of the country by the exploration for iron, and the cut-
ting of roads and trails, made this detailed study possible.

Outside of this district, however, the country was passed
over at wide intervals, so that only a general knowledge of its
features was obtained, which may be a guide to future work.
There are some interesting special results, but, as a whole, it
should be considered in the light of a reconnaissance.

TOPOGRAPHICAL METHODS.

Contour lines have been drawn for the whole area mapped,
for each fifty feet above the level of the sea. In determining
elevations the aneroid barometer was used, and sketching was
often resorted to. Valuable checks were obtained at numerous
places by hights determined by levelling, especially along the
lines of railroad.

The most varied topography was along the Giant’s range of
hills, and here, where necessary, every section line was gone
over and readings taken at short intervals. In the less varied
country north of the Giant’s range fewer determinations by
barometric readings were possible, and sketching and to some

STATE GEOLOGIST. 119

extent the use of the hand-level took their place. Much of the
territory lying south of the range is exceedingly monotonous,
so that the placing of the contour lines here was very simple.

SALIENT POINTS IN THE GEOLOGY.

Of the many varied and interesting observations which were
made during the summer, it is the purpose of this report to
give not more than a brief outline. The fuller discussion of
the various problems involved will appear, or has already ap-
peared, in various other publications of the survey, and else-
where.

1. THE GIANT’S RANGE GRANITE.

It will be necessary first to speak of the granite of the Giant’s
range, although properly, in the order of its age, this should
come after the Keewatin rocks. The granite, which is nom-
inally of the hornblende-biotite variety, constitutes a contint-
ous belt, several miles in width and upwards of a hundred
miles in length, which runs about N. 70° E. across the area
examined. The divide between the great drainage basins of
the Red river on the north and the St. Lawrence system on
the south follows for many miles this granite ridge.

Formerly, this granite had been generally assumed to re-
present sedimentary beds altered in situ, to be of Laurentian
age, and to repose stratigraphically beneath the schists (of
Keewatin age) with which it is associated. But the develop-
ments of this season’s work show conclusively that this rock,
whatever its earlier history and derivation, is in its present
position intrusive, and is younger than the Keewatin rocks.
The study of other granitic and gneissic areas in northeastern
Minnesota has in other cases led to a similar conclusion,* and
so the limits of the old Laurentian area have been considerably
reduced.

The reasons for assigning to this rock an intrusive origin are
those of the ordinary nature, and may be thus in part enumer-
ated:

1. Contacts have been found, which show the granite send-
ing stringers into the schists along the line of junction.

2. The granite contains numerous inclusions of the schists,
and of all sizes. These fragments show various stages of

*Dr. U.S. Grant, Twentieth Ann. Rep. of this Survey, pp. 35-95; Twenty-First Ann.
Rep., pp. 50-54. The probability of a large portion of the Giants’ range being of the
nature of eruptive rock was shown by Prof. N. H. Winchell in the Fifteenth Annual
Report. pp, 349, 355; Seventeenth Report, pp. 21, 30, 31, 67.

120 TWENTY-SECOND ANNUAL REPORT

metamorphism and recrystallization, which in general seem to
vary with the size.

3. -At the contact, the schists are more or less metamor-
phosed.

4. In two instances at least, the granite nearly surrounds
areas of schist, which are, however, still connected with the
main body. These peninsular areas show much greater
metamorphism than the main body. (See Plate III).

5. In T. 58-17 are two lenticular masses of granite, separated
from the main body, and surrounded by the schists. The
longest axes of these bodies are parallel with the general trend
of the main body; in mineral composition they are identical,
and in texture they correspond to the phase in the main body
which is commenest near the contact with the schists. They
are undoubtedly the surface exposures of apophyses from the
main mass.

6. Near the contact, the granite is fine-grained; but as the
distance increases, it becomes coarser and often porphyritic.

It is not possible to consider the question whether or not this
granite consists of buried and fused acid sediments of the Lan-
rentian, which by the movements of the inner crust were in-
truded among the later strata, and there recrystallized. The
northern contact of the granite with the schists, though still
distinct, is much more complicated than at the south, and this
might suggest the idea that this is nearer the ancient granitic
reservoir.

2, THE KEEWATIN SERIES.

Among the furmations mapped was a hitherto unexplored
area of Keewatin rocks, lying south of the granite belt above
described. Frequent specimens were collected here, but no
special microscopic study has been attempted. It is evident
that the rocks vary in origin, some being undoubtedly igneous,
while others have had a simple detrital origin. They are trav-
ersed by a regional cleavage which has a nearly uniform trend
of about N. 70° E., and a hade which is nearly vertical. Most
of the rocks are marked by the development of sericite and
kindred minerals, resulting in the familiar ‘‘green schist” which
has been considered the lithological peculiarity of the Kee-
watin.

Near the contact, however, as has been noted, and especially
in those positions where they are partly surrounded by the
granite. these schists have been altered into more perfectly
crystalline hornblende and mica schists. The distribution and

. : 7 Hylypiyl Sie: v
Fae 1] oath, eT sy nil I ME SHE Ul [fil ¢ /
PRE—-ANIMIKIE ANIMIKIE

Geol. and Nat. Hist Sur. Minn.

XX Ann. Rept.,. PI. Il.

oo —. OOOO“

Quartzyte Iron Bearing Member Slates

er rerr | —|
ss ————

a KEEWATIN
Green Schist Hornblende and Mica Schist

SECTION ACROSS THE MESABI RANGE.

Drawn NortH AND SOUTH THROUGH THE CENTRAL PARTS OF TOWNSHIPS 58-18 AND 59-18, THUS PASSING THROUGH THE Town Or MountTAIN LRON.

Horizontal Scale % mile=1 inch. Vertical Scale three or four times exaggerated.
This section shows the typical stratigraphy of the Western Mesabi range.

STATE GEOLOGIST. 121

relation of these crystalline schists make it clear that they
represent no distinct stratigraphical division, but are simply
among the contact phenomena of the granite. (See Plate III.)

The chief interest in this lies in the fact that the hornblende
and mica schists have in general been considered as peculiar
to a lower horizon than the Keewatin—the Vermilion or Cout-
chiching,—and their existence has been held as sufficient evi-
dence of the age of the rocks in any given case. In the dis-
trict examined, however, it appears that this rule will not hold.

On the other hand, in those parts of the Keewatin further
from the granite, especially in the southern part of T. 58-17,
there were found rocks which were undoubtedly clastics,
cleaved but not greatly metamorphosed, slates and quartzytes.

To sum up, there are in the Archean of the Mesabi range
rocks which according to their lithological features might be
held to represent three great horizons: The granites (some-
times gneissic),the Laurentian; the hornblende and mica schists,
the Vermilion or Coutchiching; and finally the sericitic schists,
the Keewatin. Actually, however, we are as yet unable to
make any stratigraphical subdivision of the Archean in this
place. In classifying the sericitic schists as Keewatin, we
must assign to the same period all except the granite, and
include the crystalline schists and the simple detritals.

The Thomson Slates.*

The detrital series, which is well exposed in Carlton county,
especially along the St. Louis river from Thomson to Cloquet,
was traced for some distance further north than before known,
into St. Louis county. The northernmost outcrop was in sec.
27, 'T. 51-19; and further north still the drift suggests that this
continues to be the underlying rock.

These slates and graywackes have been sharply folded, and
subsequently were subjected to strains which induced two sets
of regional cleavage. Of these the most prominent, and appar-
ently the first developed, varies from N. 60° E. to nearly east-
and-west. Near Cloquet, where a later dike cuts the slates, a
third cleavage is locally induced.

These rocks were correlated by Irvingt with the Animikie of
the Mesabi range, and subsequent writers have accepted this
correlation. There seems to be a preponderance of evidence,
however, in favor of considering them the equivalent of the

*Cf. ‘The stratigraphic position of the Thomson slates,’ by J. E.Spurr; Amer.
Jour. Sci., III, vol. xlviii, pp. 159-166, Aug., 1894.
+ Seventh Ann. Rep. U. S. Geol. Survey, p. 422,

122 TWENTY-SECOND ANNUAL REPORT

Keewatin of the Mesabi range rather than the Animikie, and

thus placing them below the great unconformity which is there

displayed. ‘
3. THE ANIMIKIE SERIES.

Upon the Mesabi range the rocks of the Animikie series rest
unconformably upon the Keewatin schists. To the north they
abut against the schists or the granite; while on the south they
are covered by a great thickness of drift. The exposed belt
thus follows the general strike of the strata, which in turn cor-
responds closely with the trend of the Giant's range of hills.

The observations upon the geology of the Animikie, and
especially of the iron-bearing member, have been incorporated
in Bulletin 10 of the survey. Excepting the belt above de-
scribed, no other areas were encountered whose rocks were
distinctly referable to this period.

4. THE CRETACEOUS BEDS.

The existence of certain small areas of conglomerates and
shales which from their fossils proved to be Cretaceous has
already been noted by Mr. H. V. Winchell.* These Cretaceous
strata are found only in small, isolated areas, so far as is yet
known; and these seem to be but the remains of a greater
sheet which has been stripped away by erosion. They lie un-
conformably upon the Animikie strata; and in the places iden-
tified have apparently derived most of their material from the
rocks of the iron-bearing member.

That they were laid down close to the shore is indicated not
only by their conglomeratic and shaly characters, but also by.
the presence of numerous fragments of fossil wood, which are
2 found imbedded among other materials. In one of the locali-
' ties, moreover, a conglomerate of this sort is closely associated
with a lignitic swamp deposit, showing that by a slight sub-
sidence a coastal swamp had become transformed into a sea-
beach. From the presence of these scattered fragments of
purely littoral deposits, and the absence of any rocks indicative
of deeper water conditions, it is possible that this region may
actually have been the extreme limit of the Cretaceous ocean.

5. THE DRIFT.

Two moraines cross the area examined—the Mesabi moraine
on the north, which in general follows the Giant’s range of
hills; and on the south, very near the junction of St. Louis and

*American Geologist, October, 1893, p. 220.

STATE GEOLOGIST. We

Carlton county, another, which has been identified by Mr.
Upham with the Leaf Hills moraine, further northeast. In the
nature of their composition, these two moraines are character-
istic, and yet strikingly different. That of the Mesabi range
contains boulders which, when of large size, are generally of
granite, evidently derived from the Giant’ range and the more

*extensive areas further north. The more southern moraine is
characterized by the constant presence of large boulders of the
coarse anorthosyte and other rocks which are found chiefly in
the Keweenawan province, and so must have come in a south-
westerly direction.

North of the Giant's range, as far as the Vermilion range,
the drift consists mainly of till and little-washed gravels, but
so scant in quantity that they determine the topography only
to a minor extent.

Between the Mesabi moraine and that on the south lies an
area which is nearly flat, but slopes gently toward the south.
A large part of this is occupied by a swamp, of the common

‘and well-defined variety which is called by the Indian name

“muskeg.”’* -

Where cuts have shown the nature of the soil which under-
lies the peat, it is usually of sand or stratified gravels. A large
area lying. chiefly between the St. Louis and the Floodwood
river, is composed of a uniform siliceous clay, or extremely
fine sand. This is not encumbered with muskeg.

Unmodified drift, however, encroaches upon the area in
many cases. Noteworthy ana interesting are the occurrences
in the southeastern part, especially noted between Grand lake
and the Cloquet river. Here in numerous cases cuts show a
veneer of till, with many boulders (chiefly of anorthosyte and
other rocks characteristic of the Keweenawan province), which
covers an apparently deep deposit of fine, perfectly stratified
sand. This must indicate a late advance of the ice after the
deposition of most of the drift of this muskeg area; and the
similarity of the boulders in this till to those of the southern
moraine suggests that they both may be referred to the same
episode.

*This name is distinctive, and should be retained. The muskeg supports a thick
growth of moszes and water-loving plants, and is always sprinkled with stunted
spruce and tamarack trees. In distinction from the “cedar swamp” the muskeg or
“tamarack swamp” isin the geological sense u true swamp, i.e., its soil consists of
peaty material which represents the accumulation of vegetation in shallow bodies of
standing water.

124 TWENTY-SECOND ANNUAL REPORT

The Duchess slough.

The St. Louis river skirts the northern border of the south-
ern of the two moraines described, and is thus deflected east-
erly from its previous course. In T. 50-17 it cuts across the
morainic tract and resumes its southerly course. At the bend,
near the junction of the river with White Pine creek, there is

an interesting abandoned postglacial valley. Thisis nowcom- *

paratively dry, or at most swampy, and is strongly marked for
a large part of its course by distinct escarpments. The point
of its leaving the present river channel and that of rejoining
are within two miles of one another. This old river-bed repre-
sents an ox-bow cut-off, and differs from the ordinary occurrence
in that the area enclosed by the cutoff is hilly and morainic.
It goes by the name of the Duchess slough, and is the proposed
northern terminus for the projected canal to furnish water-
power for Duluth.

a de he.

By,

LIST OF ROCK SAMPLES COLLECTED IN 1893

BY J. E. SPURR.

Most of the specimens were collected from the iron-beariug
rocks of the Mesabi range; and from the study of these speci-
mens have been derived many of the results which have been
incorporated in Bulletin No. X of thissurvey. For the nomen-
clature of these iron-bearing rocks, and an explanation of the
terms used, this bulletin should be consulted, especially the
final discussion on page 248. All the specimens from the Mesabi
range were taken from the general region included between
ranges 16 and 21.

Many of the samples of other rocks were collected with a
view to their bearing upon the problem of the iron ores; while
others had no connection with this subject. The collection is
intended to represent as completely as possible the known
formations between Carlton county on the south and the region
of Vermilion lake on the north, in ranges 16 to 21.

In general, this catalogue is to be considered as compiled
simply for convenience of reference; the rocks are indicated
by field names, which may often prove upon close study to be
incorrect, and are perhaps manifestly indefinite. No study
sufficient to permit of an accurate description of some of the
rocks has as yet been made, except in the case of the rocks of
the Mesabi iron-bearing formation.

Rocks of this series are numbered in white, each number fol-
lowed by the letter S, to distinguish them from the other series
of the survey and museum.

Cy Se A oe
‘ VES

126 TWENTY-SECOND ANNUAL REPORT

10. Gray taconyte (magnetitic) N.W. 4 N. W. ¢ sec. 3,
58-17.

11. Light gray porous taconyte, banded with magnetite.
Same locality.

12. Pale pink friable decomposed taconyte, stained brown
in places by iron oxide. N. W. 4 N. E. } sec. 9, 58-17. Near
the town of Virginia.

13. Hard lean iron ore (bematite). From the Rouchleau
(Norman) mine, near Virginia.

14. Hard green taconyte. banded with magnetite. S. E. 4
N. E. 4 sec. 30, 58-17.

15. Granular quartzyte. S.E.4S. E. 4 sec. 29, 58-17.

16. Pebbly quartzyte, decomposed and stained red by iron.
Same locality.

17. Dark green spotted-granular taconyte. S. E.48S. E. 4
sec. 30, 58-17.

18. Jointed taconyte slate. S. E. + S. W. 4+ sec. 20, 58-17.
From the face of a steep cliff.

19. Gray siliceous taconyte, changed in part to brown pul-
verulent rock. S. W. +N. W. 4 sec. 31, 58-17.

20. Siliceous and magunetitic taconyte, a pseudo-conglom-
erate. S. W. i sec. 34, 58-17.

21. Taconyte breccia. S. E. $ sec. 30, 58-17.

22. Taconyte, pseudo-conglomeratic. Same locality as 20.

23. Fine-grained quartzyte. N. W. +N. E. 4 sec. 33, 58-17.

24. Gray slate. N. H. iN. W. 4sec. 33, 58-17.

25. ‘Paconyte, heavily magnetitic. Pseudo-conglomeritic.
S. W. 4S. W. i+ see. 34, 58-17.

26. Hard hematite, coated with limonite or githite. N. W.
“45S. W. 4 sec. 34, 58-17.

27. Sideritic chert banded with siliceous and chloritic slates.
N. E. +S. E. 4 sec. 33, 58-17.

28. Taconyte slate (magnetitic) with residual fragment of
red siliceous spotted-granular taconyte. Same locality.

29. Taconyte slate (magnetitic). Same locality.

30. Taconyte slate (magnetitic), jointed. Same locality.

31. Gray jasperoid taconyte, changing to light yellow pul-
verulent rock. From the Rouchleau (Norman) mine, near
Virginia.

32. Gray jasperoid taconyte, altered in part to hard brown
jasperoid taconyte. Same locality. .

33. Green chert, with a finely brecciated band. From 8S. E.
1S. W. $sec. 8, 58-17. |

STATE GEOLOGIST. LZ.

34. Gray siliceous spotted granular taconyte. Probably
from sec. 17, 58-17, near Virginia.

35. Reddish taconyte jasper, banded with magnetite, and
showing pitted decomposition. From Chicago property, in S.
Hi. 4 sec. 4. 58-16.

36. Light gray siliceous taconyte, showing pitted decom-
position. Same locality.

37. Gray taconyte, impregnated with calcite or magnesite,
and containing a fine-grained green residual fragment. Same
locality.

38. Light green siliceous taconyte. Same locality.

39. Light green spotted-granular taconyte (green-sand-
stone?). Same locality.

40. Banded taconyte jasper, with bands of hard hematite.
From Iron Cliff, S. E. + N. W. 4 sec. 36, 59-17.

41. Dark red siliceous taconyte, with sand grains. Same
locality.

42. Gray jasperoid taconyte, changing to hard hematite,
and stalactitic limonite. S. E. 4S. E. ¢ sec. 5, 58-16.

43. Altered conglomeritic quartzyte. S. E. + S. W. 41sec.
4, 58-16.

44, Contact facies of mica schist. S. W. 1 N. W. 4 sec. 35,
59-17.

45. Mica schist. 45 paces north of 44, and nearer contact.
Same locality.

46 Actinolite (?) schist. Same locality as 45, within five
feet of contact with granite.

47. Contact of granite (hornblende biotite) with Keewatin
schist. Same locality.

48. Biotite schist, in contact with granite, as siotes From
the main contact of the two formations. Same locality.

49. Contact of small stringer of granite with the schist as
above. Same locality. .

530. Granite (hornblende biotite) from within a few feet of
the contact. Same locality.

dl. Granite (hornblende biotite), like 50. From N. HE. 4 N.
E. + sec. 7, 58-16.

302. Granite, gneissic. About S. W.4S. W.4sec. 21, 59-17.

d3. Dark green spotted-granular toaniy ts (green-sand-
stone?), in contact with black, carbonaceous shale. From the
Chicago property, in the S. E. 4 of sec. 4, 58-16.

54. Green schist, part stained brown by contact with the

128 TWENTY-SECOND ANNUAL REPORT

iron of the iron-bearing rocks. From the Hale mine, S. E. 4
N. W. i sec. 1, 58-16.

55. Mottled greenstone. N. W.4S. W. }sec. 34, 59-16.

56. Dark, spotted greenstone. S. E.4 5S. E. } sec. 36, 59-16.

57. Micaschist. N. W.4S. W. +sec. 27, 59-18.

58. Hornblende schist. About 200 paces north of 57.

59. Mottled actinolite (?) schist. Same locality.

60. Muscovite (?) schist. Occurs interbanded with 59.

61. Conglomerate, probably Cretaceous. S. E. 4 N. E. ¢see.
6, 58-17. '

62. Conglomerate (probably Cretaceous), thoroughly iron-
stained. N. EH. 4N. EH. } sec. 10, 58-18.

63. Chip from boulder of hard iron in conglomerate. Partly
magnetic, much pyritized. Same locality.

64. Red siliceous jointed taconyte, somewhat decomposed.
S. W.45S. W. 4 see. 2, 58-18.

65. Same as 64. Same locality.

66. Decomposed taconyte (pseudo-conglomerate). Same
locality.

67. Conglomerate, thoroughly ferrated and changed to
lean ore. Probably Cretaceous. Same locality as 62 and 63.

68. Brecciated taconyte, cherty and jasperoid fragments in
a spotted-granular matrix. N. W.48. W. dsec. 2, 58-18.

69. Postglacial taconyte conglomerate. From the drift, a
mile south of Mountain Iron, in 58-18.

70. Banded silica-kaolin. S. E.4N. E. 4 sec. 6, 58-17.

71. Compact taconyte gritrock. S. W. iN. EH. 4 sec. 3,
58-18.

72. Taconyte breccia. N. W. 38S. W.4sec. 2, 58-18.

73. Same as 72.

74. Taconyte breccia, showing pitted decomposition. Same
locality.

76. Dark gray impure limestone. N. W.4N. E. ¢ sec. 7,
58-17.

77. Same as 76.

78. Dark red taconyte. N. W.3S: W. j sec. 2, 58-18.

79. Taconyte breccia. Same locality as 72.

80. Same as 79.

81. Taconyte hematite slate, jointed. S. W. ¢N. W. sec.
3, 58-18.

82. Drill core of taconyte. S. E.4N. E. 4 sec. 6, 58-17.

83. Same locality. Slightly different phase.

84. Fragment (taconyte?). S. W.458. W. ¢sec. 35, 59-18.

STATE GEOLOGIST. 129

85. Taconyte pseudo-conglomerate, A decomposition phase.
Same locality as 66.
- 86. Conglomerate (probably Cretaceous). Same locality
as 82.
87. Same as 86, with incrustation of siderite (?). Same
locality.
88. Consolidated carbonaceous clay (probably Cretaceous).
Same locality.
89. Taconyte (?) shale. 8S. E. 4 sec. 9, 58-18.
90. Same, banded. -Silica-kaolin? Same locality.
91. Taconyte (?) shale. Same loeality.
92. Same. Same locality.
93. Taconyte jasper. From the Snively property, S. W. 4
N. W. + sec. 3, 58-18.
94. Massive hornblende rock. S. W. 4 N. E.4sec. 17, 59-17.
95. Sericitic (?) schist. N. W. 4 N. W. 4 sec. 32, 59-17.
96. Taconyte jasper, with disseminated crystals of magne-
tite. N. HE. 4N. H. 4 sec. 23, 59-18. Probably from drift.
97. Taconyte jasper, with coating of limonite. From the
rock-bluff to the north of Mountain Iron mine, 58-18.
98. Jointed magnetite slate (taconyte?), N. W.4N. W.}
sec. 8, 58-18.
99. Taconyte chert, changing to taconyte slate, magnetitic.
Same locality.
100. Reddish taconyte, changing to taconyte slate. S. E. 4
N. E. 4 sec. 7, 58-18.
101. Taconyte(?) shale. S. E.4N. W. 24sec. 18, 58-18.
1038. Sameas 101. Same locality.
104. Preglacial wood. From drift. Same locality as 101,
ete., and imbedded in the soft shale in part.
105. Conglomerate (probably Cretaceous). From drift at
same locality.
106. Sameas 105. Same locality.
107. Gray siliceous taconyte. S. W. 4S. E. ¢ sec. 2, 58-19.
108. Porous taconyte. S. E.iS. W. 4 sec. 8, 58-19.
109. Siliceous taconyte. Same locality.
110. Porous and siliceous taconyte. Same locality.
111. Siliceous taconyte, changing to taconyte slate, and
coated with dendrites of maganese (wad?).
112. Sideritic and cherty slate. N. W. + N. E. 4 sec. 17,
58-19.
113. Same. Same locality.
114. Same, more definitely banded. Same locality.

130 TWENTY-SECOND ANNUAL REPORT

115. Same. Same locality.

116. Same. Same locality.

117. Same. Same locality.

118. Cherty slate. S. W. 4S. W. 4sec. 17, 58-19.

119. Yellow taconyte gritrock, changing to brown taconyte
jasperoid. N. H.4S. W.4sec. 17, 58-19.

120. Gray chert, changing to porous pulverulent rock (grit-
rock). Same locality.

121. Same. Same locality.

122. Cherty slate. Same locality as 112, etc.

123. Gray siliceous tatonyte, changing to taconyte slate.
S. E. 4 N. E. 4 sec. 17, 58-19.

124. Siliceous and decomposed taconyte, with coating of
limonite. N. E.4S. W.4sec. 17, 58-19.

125. Glauconitic taconyte. From near 124.

126. Honeycombed limonite. From near 124 and 125.

127. Banded taconyte slate. Same locality as 123.

128. Siliceous taconyte. S.H.4S. E. 4 sec. 18, 58-19.

129. Taconyte chert. Same locality.

130. Same. Same locality.

131. Siderite-actinolite slate. Same locatity.

132. Same. Same locality.

133. Taconyte gritrock, with seams of iron. 200 paces
north of 128, etc.

134. Same. Same locality.

135. Siliceous taconyte, much altered to hematite. N. HE. 4
N. E. 4 sec. 19, 58-19.

136. Porous taconyte, banded with hematite. Same locality.

137. Gray siliceous taconyte, impregnated with calcite or
magnesite. N. W.1N. W. }sec. 17, 58-19.

138. Red taconyte shale. N. E.4N. E. 4 sec. 34, 58-20.

139. Cretaceous conglomerate (chiefly taconitic, much fer-
rated) containing fossil wood. N. W.48S. W. 4sec. 20, 58-19.

140. Cretaceous conglomerate, containing fossil casts. Same
locality.

141. Same. Same locality.

142. Cretaceous conglomerate. Contains pebbles of taconyte.
Same locality.

143. Porous taconyte. Same locality as 155.

144. Cretaceous conglomerate, with fossii casts. Same
locality as 139.

145. Green Cretaceous shale, with fossils. Same locality.

STATE GEOLOGIST. tal

146. Sandstone conglomerate. From large drift boulder.
N. W. 4S. W. 4 section 10, 58-19.

147. Same. Same locality.

148. Taconyte gritrock, stained with iron in bands. S. E.
4 N. E. + sec. 17, 58-19.

149. Yellow taconyte jasperoid. N. EH. 18S. W. 4 see. 10,
53-19.

150. Porous taconyte, changing to taconyte jasperoid. Same
locality.

151. Gray porous taconyte, stained with iron on the peri-
phery. Same locality.

152. Red taconyte shale. From near 148, etc.

153. Same. Same locality.

154. (Taconyte?) slate. From near 149, etc.

155. (Taconyte?) cherty slate. Same locality.

156. Taconyte gritrock, with seams of hematite. N. W.iS.
W. 4sec. 10, 58-19.

157. Gray TOD aS, changing to red taconyte and taconyte
slate. N. E. 4S. E.4sec. 33, 58-17.

158. Eainded Saeiirs slate. Same locality.

159. Gray taconyte chert. Same locality.

160. Same. Same locality.

161. Red siliceous taconyte, changing to taconyte gritrock.
Same locality.

162. Hard hematite, with limonite. N. W.148S. W. 4sec. 34,
58-17.

163. Same. Same locality.

164. Taconyte jasper, with quartz vein. N..W.4S. E. 4
see. ao, Jo—1/:

165. Same, showing prismatic jointing. Same locality.

166. Gray and red taconyte. Same locality.

167. Incrustation of chalcedonic silica, in stalactitic forms,
upon gray taconyte. S. E.4S. W. 4sec. 8, 58-17.

170. Pitted taconyte slate, N. W.4N. H.4sec. 2, 58-18.

171. Taconyte breccia. N. E.4S. W. 4sec. 1, 58-18.

174. Conglomerate (probably Cretaceous) stained red with
iron. From N. W. iN. W. 4sec. 11, 58-18.

175. Granite from contact with crystalline schists. N. E. 4
sec. 12, 60-19.

176. Schist from same contact.

177. Granite from a dike in the schists. N. EH. } N. HE. }
sec. 36, 61-19.

178. Schist from contact with granite. Same locality.

eS ee ee

132 TWENTY-SECOND ANNUAL REPORT

179. Actinolite (?) schist. From within a foot of the con-

tact of the schists with the main body of granite, in N. E. } sec.
12, 60-19.

180. Biotite schist. N. E.}N. E. }sec. 1, 60-19.

181. ‘Red jasper,” with quartz vein. From the Minnesota
mine at Tower.

182. ‘Black jasper.” Same locality.

183. Siliceous jasperoid rock. Same locality.

184. Drill cores from near Lee mine, at Tower. ‘‘Jasper.”

185. Banded jasperoid taconyte. From the Mountain Iron
mine, at Mountain Iron.

186. Schist. S. E.48. W.4sec 32, 61-16.

187. Fragment of gray calcareous nodule in slates, at
Cloquet, near the Duluth & Winnipeg bridge across the St.
Louis river.

188. Coarse gabbro. Duluth Hights.

189. Diabase (?) from center of large dike. Duluth Hights.

190. Diabase (?) from near margin of same dike.

191. Redrock. Duluth Hights.

192. More coarsely crystalline phase of same. Same local-

193. Same. Same locality.

194. Red rock from narrow dike in coarse anorthosyte.
Same locality.

195. Same. Same locality.

196. Diabase (?). Same locality.

197. Same. Same locality.

198. Red rock. Same locality.

199. Gabbro pebble, showing peripheral decomposition. .

From cut in drift, at Stony Brook station, on the Duluth and
Winnipeg railroad.

200. Slate (Keewatin?). N.W.45S. W. 4 see. 27, 51-19.

201. Quartzose slate. Same locality.

202. Schistose slate. Same locality.

208. Chips of fossil tree, found under a peat-bog, in the
glacial gravels. From cut on D.M. & N. railroad one-half
mile east of Pine station. (T. 50-16)

204. Hard hematite. Mountain Iron mine.

205. Quartzyte (Pewabic). N. W.4N. W.1isec. 36, 58-21.

206. Dark green quartzyte. Same locality.

207. Actinolite schist. S. W.458. W. 4 sec. 25, 58-21..

208. Taconyte. N. W.4N. W. 4sec. 36, 58-21.

STATE GEOLOGIST. 133

209. Glacial boulder of taconyte jasperoid. N.W.4N.H.4
sec. 1, 57-21.

210. Gray taconyte chert, changing to brown banded taco-
nyte gritrock. S.H.14N. E.4sec. 29, 58-20.

211. Gray siliceous porous taconyte, changing to hematite.
Same locality.

212. Gray siliceous taconyte, stained in part brown with
iron oxide. N. W.iN. W. isec. 22, 58-20.

218. Dark red jasperoidal taconyte. Same locality.

-214. Gray siliceous taconyte, changing to brown taconyte
jasperoid. Same locality.

215. Same as 213. Same locality.

216. Same. Same locality.

217. Glauconitic taconyte, with magnetite. Same locality.

218. Taconyte jasperoid, changing to hematite. Same lo-
cality.

219. Same as 217. Same locality.

220. Same as 213. Same locality.

221. Taconyte slate. N. E.4S. W.4sec. 29, 58-20.

222. Red taconyte shale. Same locality.

223. Green taconyte shale. Same locality.

224. Taconyte jasper. Same locality.

225. Gray taconyte gritrock. Same locality.

226. Quartzyte. S. W.4N. W.isec. 35, 58-21.

227. Actinolite (?) schist. N. W.4N. W.4sec. 35, 58-21.

228. Muscovite schist. Same locality.

229. Silica powder. S. E. i N. W. 4 sec. 23, 57-22. Near
Mesabi Chief mine.

230 Same. Same locality.

PRELIMINARY REPORT OF LEVELLING PARTY.

BY CHAS. P. BERKEY.

The party that entered upon work for the Geological and.
Natural History Survey on the 26th of June at Grand Marais
consisted of L. A. Ogaard, Alex. N. Winchell and myself under
the direct supervision of Dr. Grant. It was proposed to level
across this portion of the state to the International boundary,
to pay as much attention as practicable to the topography of
the country as the levelling advanced, and to determine accu-
rately by level such knobs or ridges as seemed of unusual ele-
vation. 'The bench marks of the level were used as primary
stations in the use of the aneroid barometer, by the aid of
which the contour lines were established. The territory that
occupied most of our attention comprises the central and
northern portions of Cook county. This was known to be the
most elevated district in the state and therefore considerable
care was taken in an endeavor to locate more accurately the
prominent points‘and ridges.

On account of the method of travelling in this district and the
extreme difficulty of running a level through such a country of
hills, swamps and poor traiis, the work had to be planned by
trips of two or three weeks duration. The first one of these
was planned to extend from Grand Marais by the old ‘‘Iron
trail” through Devil’s Track lake, Little Pine lake, over Brulé
mountain to the Misquah hills and then west to Winchell lake
and south again to Brulé lake, where supplies had to be ob-
tained again.

On a part of this first trip, which occupied the first three weeks.
of our work, we were obliged to engage two Indians, Jo Caribou
and Alex Morrison, to help in packing and cutting through the

STATE GEOLOGIST. 13)

woods. This first trip was by a great deal the most difficult
and tedious of the whole summer’s work. The trail followed
was old and abandoned, and in many places could not be found
at all, even by the Indians. The character of the underbrush
was such, furthermore, that it became utterly impossible to
use the level at all without constant cutting. Frequently after
the most diligent work, nightfall would find us little more than
a mile in advance of the former camp. But this first trip, in
spite of the enforced slow travelling and difficult work, gave, in
fact, the most satisfactory results of the whole summer’s expe-
dition. The Misquah hills proved to be the highest points
reached in Minnesota. Several knobs were accurately deter-
mined by level and many more by the aneroid, some of which
are given in the list accompanying this report

The highest point on which direct observations were taken
is between Misquah and Winchell lakes in sec. 36, 64-2 W. It
was carefully determined by barometric readings and corrected
by level bench marks close at hand, as wellas by level observa:
tims from neighboring hills. Its elevation is 2,230 feet above
sea level,—there is no greater recorded in the state. The
Misquah hills form a broken ridge extending east and west a
distance of many miles just north of Brulé river valley. A
few separated knobs also stand outside of this main ridge. But
the area in which peaks of an elevation exceeding 2,200 feet
oc-ur is very limited, Misquah lake being nearly a central point.
For a distance of three or four miles both east and west of this
lake, this hight is attained by several knobs. The more exact
position is in the southern tier of sections of T. 64, R. 1 and 2 W.

An opportunity is offered for a general view of the central
portion of Cook county here, such as can be secured at no other
place. Standing upon the bare knob of red rock just east of
‘Misquah lake, a very large portion of the surrounding country
can be seen in every direction and especially to the north and
south. The minor details are thus of course entirely over-
looked, and only important ridges bounding prominent valleys
are noticeable.

Toward the north, the general impression is that of a broad
quite uniform valley extending east and west an indefinite
distance and bounded on the north by the bluffs and ridges
along the International boundary ten miles away. In the
valley a dozen or more lakes can be seen, while hundreds more
are hid behind wooded ridges or lie in narrow deep secluded
valleys. Toward the south are three well marked features.

136 TWENTY-SECOND ANNUAL REPORT

First is Brulé river valley lying immediately at the foot of the
hills, extending east and west here also, and bounded abruptly
on the south by Brulé mountain and connected ridges. This
valley is exceptionally narrow and deep, being nearly 600 feet
below the Misquah hills and over 500 feet below Brulé moun-
tain, while the maximum distance between these two points is
not over four miles.

Brulé mountain is very prominent from this point of view.
It lacks only 60 feet of equalling the Misquah hills in hight,
and is even more striking. On its northern slope the descent
is 021 feet in less than a mile (three-fourths of a mile). In
this regard, however, it is not so remarkable as the first ridge
at Grand Marais which ascends 730 feet in a mile, or even some
of the bluffs along the International boundary which have an
almost perpendicular face from one to two hundred feet in
hight. Three miles east of Brulé mountain are three remark-
able knobs belonging properly to the Misquah hills, although
they are south of the river valley. They are near together
and have an elevation of 2050 feet by aneroid reading on the
lowest of the three. A hundred feet can safely be added to
this for the highest one.

Just beyond the crest of Brulé mountain to the south lies
lake Abita, the mountain lake of Minnesota, 2048 feet above
the sea, the most elevated:lake in the state so far as recorded.
But beyond this is the third great valley in our general view
of this part of Cook county. It extends almost east and west
as the others, but is broader and not so uniform. The southern
limit is formed by the Saw Teeth bluffs along lake Superior,
several of which appearing quite prominent seem to give a
very substantial boundary to the valley. Lakes are not so
abundant in this most southerly valley as were afterwards
found in the districts farther north and west. Swamps of no.
very great extent were abundant and often small ones occur
near the highest points. Large drift boulders are found in
abundance even upon the bare knobs of the highest of the
Misquah hills. Very little attantion could be paid to details in
any other lines of investigation.

After obtaining supplies from Gunflint City, the work of
our second trip began with topographical work about Brulé
lake. James Marshall took the plaze of the two Indians who
had returned to Grand Marais. Similar work was then carried
forward through the country adjacent to the canoe route to
Gunflintlake. Georgia, Surveyor, Ida Belle, Kiskadinna, and

STATE GEOLOGIST. 137

Ham lakes are the principal ones on the route and Cross river
is the only stream of any size. The surface slopes gradually
northward with no very high ridges after leaving Surveyor
lake until Gunflint lake and vicinity is reached. Some more
careful work was done in T. 65-4 W., especially in the southern
half of the town and in section 28 in particular. As all these
points will appear just as clearly on the maps when they are
published I will not attempt any explanation here.

The third trip of our party included towns 64,.and 65, 1, 2,
and 8 W. and was made by canoe through Loon, Mayhew,
Tucker and Banadad lakes and eastward through a continuous
chain of small lakes to Poplar lake. From this place a trip
was made toward the south through Caribou to north Brulé
lake in order to check on our former determination of level.
The return was then made from Poplar lake through Hungry
Jack, Birch, Duncan’s and Rose lakes, from which the Interna-
tional boundary route was followed to Gunflint again. The
most noticeable features of this section of country are: first the
comparatively low and uniform ridges of the gabbro belt
crowded thickly together with usually only sharp narrow
ravines between them running in every direction; second, the
bold-faced bluffs north of the gabbro belt within three miles of
the boundary lakes. All these ridges are comparatively high
and have a gradual rather gently inclined southern slope and
avery precipitous northern one. The lakes are very abund-
ant and lie in deep narrow valleys. They are connected fre-
quently by falls and rapids, as at Rose lake where the fall from
Duncan's lake is 136 feet in a distance of less than a quarter of
a mile. One of the most noticeable of these characteristic pre-
cipitous bluffs is called Rose Lake mountain. It rises from
Rose lake 470 feet by aneroid determination. The highest
points are, first a hill on the section line between sections 26
and 35, 65-2 W., which is 2050 feet, and second, the quarter post
on the north line of sec. 28, 65-4 W., which is 2038 feet. The
former was determined by aneroid and the latter by level.
Other features will be shown sufficiently well by the maps.

In the territory thus far covered since leaving Grand Marais
a few other points come into prominence by combining the
observations of the three trips. The hight of land extends in
a southwest direction from between North and South lakes to
the ridge between Ida Belle and Surveyor lakes. Lakes to the
southeast of this line drain into lake Superior; and lakes north-
west of it drain into Rainy lake. Brulé lake has two prominent

138 TWENTY-SECOND ANNUAL REPORT

outlets, one toward the east giving rise to Brulé river, and the
other to the west into Georgia lake, from which probably Tem-
perance river rises, flowing toward the south. Ida Belle lake
is the head of Cross river which flows north to Gunflint lake.
For the greater part of its course it is a chain of narrow small
lakes connected by rapids. North lake is the head of drainage
westward along the boundary, and South lake is the head of
the eastern boundary drainage, which reaches lake Superior
through Arrow river in Canada and Pigeon river on the boun-
dary. The Port Arthur, Duluth and Western railroad enters
Minnesota at the narrows at the west end of Gunflint lake and
the western terminus is now Paulson's camp four miles west.
The county road extends from Grand Marais northward to
Hungry Jack lake. During the past summer it was cut out
from near Poplar lake westward to the railroad near the west
end of Gunflint lake, and now forms a good trail from this point
to lake Superior.

The fourth trip extended from Gunflint lake westward through
Ts. 65-4and 5 W. and return through Ts. 64-5 and 4 W. There
are no features of this needing especial attention. There are
many very prominent hills, but none so high as those already
given, the most elevated ones being usually between 1800 and
1900 feet. .

After finishing this trip the entire original make-up of the
party was broken by the return of Mr. Winchell and myself to
the University. The further work was done by Mr. Ogaard,
who then joined Dr. Grant, working on the geology of the dis-
trict. And on their return to Ely the entire distance was
levelled, thus completing a very extended list of bench marks
as a basis for contour corrections in northeastern Minnesota.

Below I have added a list of accurately determined points
from the field notes of the party, and have also, with the aid
and advice of Mr. Warren Upham, drawn a plate showing two
profiles across Cook county from Grand Marais and Brulé lake
N. N. W. to the International boundary. These are each 27
miles in length and are about 10 miles apart. The one starting
at Grand Marais includes only such points as fall within one mile
of a direct line to the west end of North lake. The other,
starting at Brulé Jake, takes a direct line to the north quarter
post of sec. 28, T. 65-4 W., and then runs northeast to the
granite ridge, from which place it assumes the original direc-
tion to the boundary. (See plate IV.)

Geol. and Nat. Hist. Sur. Minn XXU Ann. Rept. Pl. Iv.
, a Giant's RANGE . |
+-2,000 feet. g |
\ ‘ ‘ 1 i / i

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1 S.'S.E. | ! a Ny 1 yy oI fi
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t : Ao ee Snilea e e oe 5 i Ee eee oe ae) ena ae eee Tee ee Jom

Two Proreugs AGRISS COOK COUNTY,

rrom Brute LAKE AND FROM GRAND Marats N. N.

1 ae eae

W. To THE INTERNATIONAL BOUNDARY.

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fre =. w i i r > ede Was A

STATE GEOLOGIST.

139

The following points are of sufficient prominence among
those which have been accurately determined by level to war-
rant giving them a place here for future reference:

Feet above

the sea.

Mevil’s Track lakewaweo.. i. 1636
Mnbple Pine lake... sesee sie « 1837
lia beHoot lake)... c50%.c i. se.02 1885
ACP LING SU DCC.5 a als ticle cictate sia oshs ads 1920
[DBIR@ OO eee an dnc cers meeeoe 2048
PESTA CHOU UM bal Meshete ta «12! o> <hoie's-« 2170
MATATLGH ERT VET LAROSE. 5 is: o\ei ele s-oreies 1649
MithevEroutlakecss. 2os2%6% 6 1910
Ridge S. of Little Trout lake. 1994
Misquah Jake. - .. 5... 62+... 1911
Hill E. of Misquah lake. ..... 2223
OTIS SHANG Ber eevee seid sss dais lowers 1866
WVOEDMABTUILE AKER: 5 5c ac eels os 1854
PAGAN ASAKC : cia csise ed aes 1878
WaemellewlAlkG vizs.clecs sie bees acer 1910
Hill S. of Winchell lake in

Reed OA=Oi WV simicic'e ee 0 s0in ate EPA
PMN LAKE. 8. sss ws Abe Gre 1915
2 fll So ORG ais ae eee 1851
MRR OM ANTEC) reat sie 54 oislale aue-neielers 1841
Hill at W. end of Brulé lake,

iar ion Gao We re cheiscie) craic cisielers 2084
Surveyor Nene ee es Sard eersras 1849
Makertda Belle .o..2.0c.s0 22%. 1794
DNeinvow Wake.6.) 5-08 Moca bees 1782
RGIS AGM MA LAKE cco sci ele aisle 1767
WIGAN ALIS@ yee ccs hedas aie sie s 1706

North + post of sec. 28, 65-4 W. 2038

See AK Cte. <0, tetas once es 1547
HSIAO Aa ie sie eencs saad ais 1745
MVE WAKO) 515.2 Scat isials sie: aes’ 1853
ISGanVeie AKO. 28 fe Soe syste ere ss 5 1880
BIS @MOCTMI AKO © rc<s aoe aiasroie oe e's 1847

Feet above

the sea.
anadadlakesn: actassocseee a 1944
Istlake E. of Banadad lake... 1942
2d lake E. of Banadad lake... 1927
3d lake E. of Banadad lake... 1927
Poplarilakes costs oe qaeteee soe = 1859
Sbraightilake: ... %itee.- yaaa 1879
Caribou lakes. oscinde ces betas 1868
Mieeds lakes ot: Ae fats nice tee ais 1879
Euneny Jack Wake. 77st. sen) 1687
Birchialake@s 23 35 oF eccutercrcee 1684
Manrelisnla Kenton foyaskseise aaa 1684
Duncan’ silakes a actos sacs ere 1664
NOS CHK yo seth ects eae 1528
Ha Gabaikee ey. wn ccicle.e Seed deere 1531
SS Otel allKewes chat cies a chereiste tees oe 1558
INGOrbhnelake seas hives wowmcres. 1550
Little Gunflint lake .......... 1548
AKCLeY PAK BR siietsansirs cts storstees 1779
IPaulsonesmaker sss adna. sete er 1708
Black Trout lake (Kakigo lake) 1663
Bashitanagueb lake.......... 1657
Peter lake (Clothespin lake).. 1608
Gabemichigama lake......... 1587
INEPVINON AEN Bes ca cBon So Bdoeber 1585
Little Saganaga lake......... 1600
Muscovadormlakerson ses soriees 1706
Greenalalkete sie gak occ tee ater 1730
GalterMiakel. s2i..5. 42 Stee seee es 782
Charleyslakewc. x. sseose cents 1763
1 BYS12 7 ya en ce ss ORE Tar te 1748
lying: 6loudwlake ss. cscs 1738
Greenwood Island lake....... 1641
Hast and West lake........:.. 1618

The following are on the canoe route from Gabemichigama

lake westward to Ely:

Feet above

sea level.
TETORETIY ceI ae ar 1539
Ogishke Muncie lake.......... 1488
NOTED KGS Sais oes levers oie ble e/a ercle's 1491
CI RE Rao SRO COS Een Er 1490
Epsilon lake...... Eaererct Mice Vera ee 1460
WO MAKES, te aialc a nous cies eee 1469
eMC mele oncclea cece «6s 1470
TENB TP GW) laine Oe Pn eg 1475
PROMT AGIA ICC. ols. cioais oe ac.ale + 1495
Kekequabic lake.............. 1497

Feet above
sea level.

ASCO RGr Nye orete a ath rope) otohete: ne ai 1381
Ist lake west of Knife lake.. 1371
2d Sade IBLOL
aig pee “s ss SO aes alata
Carp takes cciacls stactce sto oosiastes 1355
SuCKe Rakes esac core sldeicrea: 1330
Basswood or Bassimenen lake. 1300
INGwitonmelakessc-s> cos scieee o 1307
PENMAN ei po paeca s cceast ae oneal ota are 1313
NOIR AION stave ret Sores arelo'colleisie(orsiers 1337

140

TWENTY-SECOND ANNUAL REPORT

The following are a few points of prominence determined by
barometric readings and corrected by level bench marks:

Feet above
the sea.

South Devil’s Track lake......
Knob S. of Little Pine lake...
Knob 3 miles E. of Brulé Mt.,
SOG, (24 63-1 WW oricele crs cee
Hill N. E. of Little Trout lake 2023
Hill, sec. 36, 64-2 W.,at Winch-

Ol) Iakes.): Csi. .i veka Sete 2230
Ridge S. of Brulé river,sec. 22
GW. diets eich ees & aie ee alec 2027

Granite ridge sec. 14, 65-4 W.. 1967
Ridge south in sec. 23, 65-4 W. 1942
Mea Gull lake, scents oc 1440
Ridge S. of Gunflint ge sec.

2b AGD=45 Ws. or. ene Saisie 1892
No-name lake. RR HA AM Oy aes eae 1787
Portage Jake's evs cee 1872

Feet above
the sea.

Hill 8. of Hungry Jack lake,
sec. 3, 64-1 W

Moss lake.

Knob south of Duncan’s lake. 1907

Ridge between Duncan’s and

eee ewes wwe e we eene

Roveljlake...20. as pean 1947
Rose Lake mountain.......... 1997
Hill, see. 31, 65-5 Ws... sense 1827
Hill, see.-29, 65-5 W. vaocee eee 1867
Little Round lake............ 1677
Little Copper lake............ 1777
Lake, sec. 15, 64-4 We. .ecee 1867
Hill ¢ mile west of this lake.. 1967
Snipe lake..if0.3 39% Ss, woe 1757
Burnt hill north of Snipe lake 1927
Big Round lake: 23..5.)5-neeeee 1702

oy et

XII.

PRELIMINARY REPORT OF FIELD WORK DURING
1893 IN NORTHEASTERN MINNESOTA.

BY ARTHUR HUGO ELFTMAN.

CONTENTS.

Page
Ser TEPPEC TION Fy. Oly LLGIGL, WORE! nose coolers fo lcis soe a's ee dele sore ahd e Sle! dhe ulghein den 141
Sip, Ruan a tile VIRAGO rd srseroos vy ska nls ou abd awe’ s etoctalel ne Gabe/olae Oa Bed 141
MEPS ROMLES Olabravel Int Make lGCOUNEY: sac sss 5 books ebook back 143
nee sHconomicmresources: of lake County. 2 ..¢-.<0-2+-ceccscnnen 146
EMAILS S eet tee oso 5 nk clare eeeee J4.o.c'e te « koe we ee 146
V. Map of west-central part of Lake county......... pastas sya 1£0
Geological notes on northeastern Minnesota................ ccc ce eeee 150
INR ANTITE BIG aes te 2 aeheis s ors.x Acoli s ae Seeder t co tects aS 150
MDa SELOLWNELIG (UBICG ATES ooo <)5a!s 55 ofore sie aise sls fied bo oi Saale hed Co Od « 151
Repionm north ol the lake. .ccesch wrceasen : Sie thal ss 151
BIRDIES TAU LGCSi i a sea kicladis omyartiddore ees Pte Me est cton wales 155

Ill. Actinolite-magnetite schists from the eastern Mesabi
(DIVE) Ss epee SEO) CORO IOS SA een tL AR CORIO Se HOCCIOIO AES 159
Specimens collected by N. H. Winchell............ 160
Specimens collected by H. V. Winchell....... ..... 162
Mpher GUSEHV AION! t Wass rents Se ates x ohn docs e's 166
SS NTOLEDE 97S Re aie Cie PR eee ae PC (a 168
RNR LINED «fs vibe micinlte cd Selah Gages we dialed amin need ows bale ye 169
Bem SEI PCUE ROCKS «5c ccarai ies ate ono om ae Peta aa we oo acs ns Ges oo etn 170
ee MONA DASE << eas oh oe Hara) wip ois ceale tala Pelee wa cl b ewe bweeiea 173
VII. The anorthosytes of the Minnesota shore of lake Superior 174
SMM SITTPIINIAT Yc. «(5502 ois ows ae he ows jesence FF Te) PE eG 179

GENERAL REPORT OF FIELD WORK.
I. REGION TRAVERSED.
The territory assigned for investigation was ranges 8 to 11
(inclusive) west of the Fourth principal meridian between the
latitude of Ely and Snowbank lakes and the shores of lake Su-

“0 ee eee

&
¢

142 TWENTY-SECOND ANNUAL REPORT!

perior. The writer, accompanied by Mr. H. HE. White, as
assistant and topographer, and Mr. B. F. Merrill, left Ely May
4th and spent the first week in making observations around
White Iron lake. As soon as theice had sufficiently broken up
to permit canoe travelling, a trip was taken up the Kawishiwi
river, north through Triangle, Moose, Snowbank and Disap-
pointment lakes. Snowbank lake, excepting a narrow passage
along the south shore, was covered with a field of ice. The
work assigned on this lake was thus postponed until later in
the season. Wilder lake completes the list of lakes examined
during May. JDuring June the region around the south Ka-
wishiwi and Isabelle rivers was examined.

Some of the important lakes which were geologically
reviewed and investigated, are Isabelle Trail, Bald Eagle,
Gull, Gabbro and the eastern end of Birch lake. An overland
trip through townships 60-11 and 61-11 was taken during the
latter part of the month. The work was considerably hindered
by the great forest fires upon the Mesabi range. The north-
western part of T. 60-11 was swept by the fire and the
Stony river marks the eastern extent of the great conflagra-
tion. Numerous other fires were started by careless campers
and large quantities of valuable timber were destroyed. Dur-
ing the hight of the fire the sun was obscured by the smoke for
several days.

In July a trip was taken up the Stony river to Sand lake
(T. 59-11) and to the center of T. 59-9. This river is so named
on account of the large number of boulders in the stream,
which greatly hinder and even make canoeing quite danger-
ous. From the Stony river the work was transferred to the
south branch of the Isabelle river in T. 60-9. Heavy rains
filled the streams and made travelling comparatively easy on
the rivers, but almost impossible through the swamps. Owing
to the unexplored condition of this region it was necessary to
cut a number of portages. A canoe route was made from
Smokehouse lake (sec. 28, T. 60-9) to Clear lake in section 14
of the same township. This makes a complete connection of
the three principal canoe routes used in reaching the head-
waters of the streams flowing north. From Clear lake we went
down the south Isabelle river and returned to Ely. After get-
ting supplies, several days were spent on Snowbank lake to
make the observations which were postponed on account of the
ice during our first visit to this lake.

STATE GEOLOGIST. 143

We went up the south Isabelle river toClear lake, from which
a two weeks’ overland trip was made through townships 61,
60, 59 and 58 of range 8. This was by far the hardest part of
the summer’s work. The region around Greenwood lake was
next examined. The prominent elevation south of the lake
was called Greenwood mountain. It is an oblong ridge about
a mile long, extending in an east and west direction, a mile
wide at the base, one half a mile across the top, one hundred
and fifty feet above the lake and the surrounding country,
which is nearly level and has an approximate altitude of 1850 feet
above sea level and is covered with a. heavy growth of green
timber. From Greenwood lake it is the only ridge visible, and
can be readily recognized by its peculiar form from the high
hills at Disappointment lake, fifty miles north, and from the
ridges around Beaver bay, seventy-five miles southeast. Green-
wood mountain marks the most prominent western outcrop of
the group of rocks called ‘‘red rock” on the map accompany-
ing this report.

The examination of townships 58-11 and 57-10 and 11
was completed by the first of September. During the
months of May, June, July and the fore part of August the
supplies were obtained at Ely. In Augusta trip for supplies
was taken down the St. Louis river to the Duluth & Iron Range
R. R. and thence by rail to Mesabi.

On September 2d the headquarters were transferred to Two
Harbors and Beaver Bay. At Two Harbors Mr. John Bean,
an experienced surveyor and one well acquainted with the
region to be examined, was employed in place of Mr. White,
who left for Minneapolis August 23d. Three weeks were
spent in the vicinity of Beaver Bay. Special attention was
given to the relations of the anorthorsyte to the other rocks.
Three excursions were made north from Beaver Bay to con-
nect with the work carried on from the north during the fore
part of the season. The remainder of the season was spent in
working north of Two Harbors.

On October 20th the work assigned for the season was com-
pleted and the party disbanded.

II. ROUTES OF TRAVEL IN LAKE COUNTY.

The different routes of travel by which points in this region
- are made accessible will be given in groups under the places
from which they start.

144 TWENTY-SECOND ANNUAL REPORT

Ely Routes. The canoe routes along the International boun-
dary and the Kawishiwi (Cashaway) river are well known and
need no description. The Isabelle river route follows the
Kawishiwi river to the portage in sec. 30, T. 63-10, passes
through Clearwater lake to the south Kawishiwi river in sec.
32, T. 63-10, and then through Gabbro and Bald Eagle lakes
and up the Isabelle river, which flows through the southern
tier of sections of T. 62-8 and 9, to Isabelle lake in the south-
eastern part of T. 62-8. The main stream of the Isabella river
crosses the northeastern part of T. 61-8, and comes from Bel
lissima lake in the southeastern part of T. 61-7.

A short distance east of the portage in the centér of sec. 34,
T. 62-9, is the mouth of the south branch of the Isabelle river.
This river, although of considerable size, spreads out near the
mouth into low marshy ground and is almost wholly con-
cealed. It flows in a zigzag manner in a northeasterly, direc-
tion through T. 61-9, and in T. 60-9 it flows in a southwesterly
direction. The river is canoeable to the lake in sec. 15, T.
60-9, from whence a portage is crossed to Clear lake in see. 14,
on another branch of the Isabelle river which flows northeast
from there, and is not canoeable. From Clear lake trails con-
nect with the Mesabi and Beaver Bay trail, and trails running
through T. 60-8 and T. 59-8.

The Stony river route from Ely is through White Iron and
Birch lakes, then up the Stony river which empties into the
lake in section 380, T. 61-11, in a concealed bay nearly a mile
long. From Birch lake to Slate lake the river is full of rapids
and numerous portages must be crossed. The fall in the river
through this distance is about 230 feet. On account of the dif-
ficulty experienced in going up the river to Slate lake, this
part of the route is seldom used. The Harris lake route or the
‘*60-10” winter road is taken instead. This road leaves Birch
lake in the narrow bay in sec. 20, T. 61-11 and reaches Harris
lake in sec. 27,—a distance of three miles (6,000 paces).
Harris lake is 170 feet above Birch lake. From the east end
of the lake the road runs southeast to Slate lake a distance of
four miles, and follows the Stony river to Pike lake in sec. 36,
T. 60-10. A portage from Pike lake goes to Smokehouse lake
and the Isabelle river. At ‘‘Headquarter camp” in the center
of sec. 21, T. 60-10 a short trail runs east through the center of
Towns. 60 10 and 9 and crosses the southwest corner of T. 60-8.

For the portages on the Isabelle and Stony rivers, see the
list of altitudes given below.

STATE GEOLOGIST. 145

Mesabi route. This trail leaves Mesabi station, follows the
Masabi range to the north town line of T. 59, and continues east-
ward along the same line to the northeast corner of T. 59-8
where it crosses Beaver Bay trail running northward. From
here the trail continues southeast and eastward to Pork bay on
lake Superior. Minor trails run north and south from the main
one at different points. This is not a canoe route.

St. Louis river route. This route leaves the Duluth and Iron
Range R. R. at the St. Louis river and follows the river nearly
up to its source in T. 59-11 and then by a portage four miles
long crosses to Sand and Stony lakes and the Stony river, or
from Sand lake to Greenwood lake.

Cloquet route. A trail leaves the railroad at Cloquet river and
runs to the north line of town 55 and east on the line to the lake
in the northwest corner of T. 55-10. From here a good trail
runs north to the two lakes in sections 29 and 31, T. 56-10 and
east along the north line of sections 28, 27 and 26; then it takes
a southeasterly direction to the northeast corner of sec. 35, and
' thence eastward across T. 56-9 to the Beaver Bay and Green-
wood lake trail.

Highland route. 'This trail leaves the railroad one mile north
of the station and is easily followed. In town 55-10 it has num-
erous branches and connects with the Cloquet trail.

Two Harbors trails. The county road runs along the lake
shore from Duluth to Grand Marais passing through Two Har-
bors and Beaver Bay. A trail leaves Two Harbors and follows
the line between ranges 10 and 11 north to the Highland trail.
A number of minor trails leave here, but it is unnecessary to
mention them as they are well known. From Two Harbors to
Beaver Bay the usual route is by steamer.

Beaver Bay routes. Besides the county road there are several
good town roads which run north into T. 56-8 and west to T.
55-9. From the end of the road in sec. 27, T. 56-8, a trail runs
to Schaff’s lake in sec. 12 and from the east end of the lake
follows the range line north to the northeast corner of T. 59-8

where it connects with the Mesabi trail. The trail does not
ollow the range line very closely, but runs about one-half a
mile east of it. The Greenwood lake trail leaves the town road
in the center of sec. 9, T. 55-8, and runs nearly northwest to
Greenwood lake twenty-four miles from Beaver Bay. An old
and indistinct trail follows the line between ranges 9 and 10,
between the Mesabi and Greenwood trails. A portage four

146 - TWENTY-SECOND ANNUAL REPORT

miles long connects Greenwood lake with Sand lake. Im sec.
25, T. 56-9 the Cloquet trail connects with the main trail.

Among other trails which run north from lake Superior those
following the Split Rock and Gooseberry rivers and the one on
the line between ranges 9 and 10 are the only ones deserving to
be mentioned. In T. 55-9 are a number of trails which connect
with the more important ones given upon the map.

Ill. ECONOMIC RESOURCES OF LAKE COUNTY. ,

Upon this subject not much can be said. In the northwest-
ern part of the county are numerous outcrops of iron ore, but
beyond a few diamond drill sections, nothing has been done
toward exploring and mining the ore bodies.* Towns 61 and 62
are nearly wholly within the gabbro area. Both of these
towns are absolutely worthless, being covered with bare knobs
of granite and gabbro, and with swamps in the valleys. Town
60 has a large amount of valuable timber, mostly white and
Norway pine. The greater part of this when cut will be taken
down the Stony river and thence to Fall lake, where a saw mill
is in operation. Towns 59, 58 and 57 have scattering patches
of good timber, but on account of the small quantity scattered
over so large a region, and the inaccesibility of the same for
the present, this has but little value. The greater part of
these towns is covered with ‘‘muskeg” and almost impassable
cedar (‘‘tanglefoot”) swamps. In T. 56 there is a large amount
of good timber, the greater part of which is not yet large
enough to be cut. T. 56-8 has considerable farming land. In
Ts. 55-10 and 11 and 54-11 there is considerable timber which
is widely scattered. The towns immediately back from the
shore of lake Superior have good hay meadows and agricultu-
ral land. That farming can be successfully carried on in this
region is shown by the flourishing farms around Beaver Bay.
The region is not very heavily wooded. Maple trees are quite
common.

IV. TOPOGRAPHY.

The topographical work consisted of drawing contour lines
for every fifty feet in elevation above the sea level and the de-
termination of the altitude of all prominent places. An ane-
roid barometer was used to determine the altitudes. Especial
care was taken in obtaining the hights of the various lakes and

*H. V. Winchell, 17th Ann. Rep., pp. 120-127.

STATE GEOLOGIST. 147

rivers along the more common routes of travel. Whenever
possible the altitudes determined along these separate routes
were checked with each other in order to eliminate any errors
which might have arisen. The fall over rapids in the rivers
when less than five feet was estimated.

The mapping of plates 78 and 79, embracing Ts. 61-10 and 11
62-10 and 11, and Ts. 62-8 and 9 and 63-8 and 9, respectively,
was completed.

In Ts. 64-8 and 9 the region around Disappointment, Snow-
bank, Ensign and Moose lakes was mapped in connection with
the geological work.

In the region south of plates 78 and 79 and north of the water
divide between the streams flowing into lake Superior and those
flowing northward, the principal determinations were along the
Stony river to its source in T. 58-10; the Isabelle river and its
southern branches; St. Louis river from the Duluth & Iron
Range R. R. to its source in section 17, T. 59-11. The alti-
tudes along the main lines were computed from the mouth of
the rivers toward their source, and were checked at the follow-
ing places: Seven Beaver lake on the St. Louis river to Sand
lake which is tributary to the Stony river; Pike lake (sec. 36,
T. 60-10), a widening of the Stony river, through Smokehouse
lake (sec. 28, T. 60-9) to the South Isabelle river in sec. 27, T.
60-9, and then to Clear lake in sec. 14, T. 60-9 on the south
east branch of the Isabelle river.

Region around Beaver Bay.—The work is this locality was
carried on from lake Superior toward the interior and connec-
tions were made with the work on the north of the ‘‘divide.”
Ts. 85, 56, 57 of ranges 8 and 9 are included in this area.

North of Two Harbors.—The measurements taken in towns
52 to 56, inclusive, of ranges 10 and 11 are only approximate
and in some cases are merely estimated.

The following altitudes or the more important places deter-
mined during the season’s work have been corrected by Mr.
Warren Upham and the writer. The fall in the rivers at the
various rapids depends entirely upon the amount of water in
the river. Ina number of instances the short and low rapids
disappear in high water, while in low water it is often neces-
Sary to drag a canoe for several miles through shallow water
and continuous rapids.

148

TWENTY-SECOND ANNUAL REPORT

Altitudes in Feet Above the Sea.

Determined by aneroid barometers; excepting several lakes
‘designated by asterisks (*), whose hights are known by level-

ing:
Feet
Hall lakes: Scemeaa tcc eens 2*1313
Garden or Eve lake........... *1384
MATIN MAIC. Soe setiers acces totes 1386
Wiitedronilake so s)aoc¢ eee 1395
Birchlake: se. hte. Stes 1410
Oopeland’s Jake....: 5.0... 22.5. 1425
Fork of the Kawishiwi river,
Sec. 26) 263-108 saat ees oe 1435
‘Crab lake and northeast elbow
of Kawishiwi river in sec. 15,
TDG SAO ae etree foe ae 1471
Ridges about 4 mile north of
the Kawishiwi river. in the
northwest part of T. 63-9,
PMDOU Gis. tee Bee REND coat e es 1730

Large lake on the Kawishiwi
river, in the southeast part
FAURE I 1491

Lake of Kawishiwi river, sec.

Soe OS Ore ae ce es SS 1520
Wailderlakes ut ccs ee ee ot 1540
NA OPALICOPVYE s hiccse rece mee 1544
"Triangle lakecocbsiws seks 1490
North UT winlake: 222. ceeee 1475

Bassimenan (Basswood) lake.*1300

Suckemlaker: hs tees eet ace 1330
New Hound: lake. 54 faces 1331
Windata kere. e toecee ie eee 1359
MOGSONAKG’ Sica: ose soe eae et 1339
I PADOT ANCE. eda a gals See *1387
Snowbank lake.725-.-okidsioe *1424
Masion “Makes: 0.5.5.) s0 free *1342
Disappointment lake......... 1499

Feet.

Disappointment hill, sec. 35,

T. 64-8. about 1 mile east of
thisttake : 4.2 5..<2°5.%: ene eee 1850
Gabbrouke.... ..ceceseee eee 1464
Bald Eagle lake ..... insjedde’ Geete 1468

Lake on the Isabelle river,
secs. 29 and 32, T. 62-8...... 1533
Dake Isabelle:,......: ¢ Spee 1570
Bellissimadlake ... 0. Jose eure 1650
Harristakes.. 2: eee 1580
Slatetlalsewss. 4). Sa. sitet oaeeee 1640
Stony sake eeu. st cece es eer 1668
Sand lakes aa sc ie eee 1674
Greenwood lake.............. 1705

Greenwood mountain, sec. 30,
T.58-10, about 14 miles south
of thisilakest=. a> seessoneae 1850
Lakes in the west part of T.
59-11, at the head of the St.

Louis river (of. 5. acne eee 1685
Seven Beaver lake ............ 1675
Pine: lakes oe és isin cee 1705
Pike lakes3i. hs od. eee 1700
Lake in sec. 22, T. 59-9 ....... 1745
Muck lake, at the head of

Stony Liver. wo. ceee see 1755
Smokehouse lake............. 1740
Clearlake on 20232 See 1704
AGanishlakerts soe ahve Jape 1800
Schait’s’ lake czscic) cocci 1089
Bear’ lakes. i...) i2 tet sere 1160

Lake Superior, mean,
1888, above mean tide sea
level) 3.24: ue tL ee

Portages on the Stony river.
From Birch lake (1410 feet above the sea) to Slate and Pike

lakes and the lake in Sec, Puy tak bie 5} § a Oo

To alti-
Ascent tude

No. Length. Location. in feet. above
the sea.

Ler Vex rete: S. see. 30.:T. 61-11 ae. eR eet Syeda 10 1420
2) .¢mile’..2... Na Hid Of N.B.:2;\sec. 31, 2. GIEM on neon 20 1440
3 1 TOC ate is eerste SW diGf IN. HP sec. Sl. ent eee coe 1 1441
er Mer ae eAee es N. part of S. E. 2, sec. 31, 'T. 61-11-02... 6 1447
Dares AM ULe Le? aye Crossing south line of sec. 31.............. 24 1471
Gages Mei ay. INWES2 OL see 3, SCC. Ota OO mle bremere sis 15 1486
fe VOU TOS: etre ING OW oa Ok NG W 4, ROCKO MACOS epee ie. 20 1506
Seba WANG een W. 3 of 8. 'W.2, sec. 8, T. GOAL... ious ss. 69 1575
9. tmile .S. W. t+ of N. E a Sec. 17, DA60= ae toc cee 15 1590
Osi Ie) hoes North. oes of S. W. 4, sec. 16, T. 60-11... 5 1595
Tannery. Ss: Wc Of Be Be 4, Sec) 165 60-Mie. Sec. 7 1602
TZN ES TOUS cies Se WiatsOl gos WVV sits SOC 10, TP, GO=11 .herats 5 1607
13. mile, | S25. Central part of sec. 10, T. cia haa ACG La 5 1612

—

14.

Shortrapids.

te mile’. 3;
ATAIIG i hie

=e MINE. so

Short rapids
ACME Ae:
ATIVE Kfar es
Current and
Current and

STATE GEOLOGIST.

N.W. 4 ofS: HE: ¢,:sec. 10; I. 60-11 .....-:. 2
The usual portage instead of the last three

is ? mile long, from the N. W. corner of

sec. 15 to the N.W. 4 of the S. E. + of sec.

E. part of sec. 11 and W. part of sec. 12... 10
Ee OMMSE Gentz ed COMM. te cae oAeocie were nes 10
Current and rapids to Slate lake.......... 6
he E. part of sec. 17, T. 60-10, to Chub

DYESS 015 DEED OY Ob AT EES OCT ORI RI TE ees 15

S. E. through N. W. 4, sec. 21, to Stony
river at Headquarters camp, near the

GeMher Oly WIS|SCCHION «=. soos. 5a neice ~cifeie « 10
N. W. 4, sec. 34, T. 60-10, to Stony geese 3
Crossing N. W. 4, sec. 35, to Pike lake . 32
S. 4 of sec. 31, T. 60-9 Aer Rn RS nea rok Fe 28
rapids to lake in sec. 8, T. 59-9 ........... 11
rapids to lake in sec. 22, T. 50-9 .......... 6

Portages on the south branch of Isabelle river.

149

1614

1624
1634
1640

1655

1665
1668
1700
1728
1739
1745

In ascending the Isabelle river from Bald Eagle lake (1468

feet above the sea) a portage about a half a mile long is made
in sec. 5, T. 61-9, with ascent of 50 feet, to 1518; and two short
portages successively ascend 2 and 5 feet in the south part of
sec. 84, T. 62-9, to the north of this south branch, near the
middle of the east half of this sec. 34, at 1525 feet.

4
°

(OAD OME CO DO

Length.

HOTOESS. oo:

+ mile.

Ascent
Location. in feet.
poy Vid heat a eae ed WR ES 5 a eo 1
Saks Mina Ob Ne aW ier SCL Oy te, GIRO: Fo7, boas 3
ING s2ONSCC el Gtr Ol= Oly te c\araloecsaaleeiers sieve oe 4
Pea a Or SCO 1 Osa GORA eS hecice con Fae 20
We WW ere Set SOG: 29 obs GIO: Laos. 5
N. E. 3 of N. W. #, sec. QO RTE AG Oe ee antes 4
N. part of S. W. 4, sec. 29, T. b1- Nea ed Fe 8
Near the center of the S. W. 3 7, Sec. 29%: 6
eaosh Win COLDEH Ol SCC 429. sult O19) ces masiecateiol= 7
. + of sec. 32, T. 61-9, T. 61-9. LSE idem ator 45
W. tof S. W. 4, sec. 5, T. 60-9. sia erore le 15
JW seGrnenose see: 85 T.. 6029's... soca). sles 3
E. part of N. W. 4, sec. 8, to a small lake.. 14
S. E. corner of sec. 8, T GOT AS SY «3 5
Vie MSC CMO y OMe 60 = Oras oti a iucse lave ee alors 15
S. E. 4, sec. 9, and SomVVierts SeGs 105, 1 6029) 20
W. edge of S. E. 4, sec 10, to lake in the N.
E. + of sec. 15, T. 60-9 Pere taa odie idicteiaie hole ate t
From foregoing lake through N.4of sec.
ia 60-90) torOlear lakes. a4. [o9e8. 0

From Clear ‘lake southwest to the South
branch of Isabelle river in the south .
edge of the N. E. 4 of sec. 22. T. 60-9.... 20

IN. edge of. S. H..4, Sec. 22, "TE. 60-9........0<. 7

Central part of S. E. 4, sec. 22, T. 60-9, to
lake on the south line of this section....

.-.From foregoing lake southwest through

GhHeeN WwW . + Ole SeGe ov, Eo 60:7 Re 9; to
SIM OME OUSCH AK Gy .jottec ciclo heise heceete ie ares 2

To alti-
tude
above
the sea.
1526
1529
1533
1558
1558
1562
1570
1576
1583
1628
1643
1646
1660
1665
1680
1700

1704
1704
1724
1731
1738

1740

150 TWENTY-SECOND ANNUAL REPORT

Y. MAP OF THE WEST-CENTRAL PART OF LAKE COUNTY.

The map of the west-central part of Lake county which ac-
companies this report comprises townships 55 to 61 inclusive,
of ranges 8 to 11 inclusive. Nearly one-half of this area is
still unsurveyed. The surveyed townships excepting the
southern tier of towns, T. 56-8 and T. 57-11, were surveyed
within the last two years, The plats of the unsurveyed parts
were compiled from data collected by the writer. The town
and range lines have been run through this region and all
points were located by pacing and running by compass from
known points on these lines, In order to guard against errors,
all necessary corrections were made in the field. The follow-
ing towns are not surveyed: 61-8 to 11, 60-8, 59-9 and 10, 58-8
to 11,* and 57-8 to 10. Trails and portages are indicated by
dotted lines and were fully described in a preceding section.
The geological boundaries are indicated by the continuous
lines drawn between the words gabbro, red rock and diabase.
These terms are used as convenient designations for the three
large groups of rocks included within this area, and will be
explained in the geological part of this report. (See plate V.)

GEOLOGICAL NOTES ON NORTHEASTERN
MINNESOTA.

I. INTRODUCTION.

The notes contained in the following pages are based upon
observations made for the state geological survey. The labo-
ratory work has been carried on in the laboratories of the de-
partment of geology in the University of Minnesota. Over
three hundred thin sections have been made from specimens
collected for the greater part by the writer. Lack of time,
alone, prevents a.more extended account of the observations
made from being given at this time. The writer hopes in the
near future to give in fuller detail the results of further exam-
ination of the Keweenawan eruptives of the north shore of lake
Superior. In giving the township and range in these notes the
township is always north, and the range is always west of the
Fourth principal meridian, Minnesota, unless otherwise stated.

The writer desires to express his sincere thanks to Prof.
C. W. Hall, of the University, and to Prof. N. H. Winchell and

*Since the above was written plats of towns 60-8 and 58-10 and 11 have been received
from the Surveyor General.

Geol. and Nat. Hist. Sur. Minn. XXII Ann. Rept., Pl. V.

R. VIfI Ww.
W

4 of Isabelle

MAP OF THE WEST CENTRAL PART OF LAKE COUNTY.

STATE GEOLOGIST. 151

Dr. U. S. Grant, of the geological survey, for kind assistance
given throughout the investigation.

Il. SNOWBANK LAKE AREA.

Region north of the lake.

Observations on the rock outcrops on the shores of this lake
are found in the 15th, 17th and 20th annual reports of the sur-
vey. The writer’s attention was directed to the hitherto unex-
plored region extending from the north shore of the lake to
Moose, Newfound and Ensign lakes. Between Moose and
Snowbank lakes five cross sections were made. On the south
shore of the former lake the rocks are sericitic and argillitic
schists. The range of hills extending parallel with the lake
shore is composed of vertical beds of schists, argillyte and con-
glomerate. South of these hills, at points from one-fourth to
three-fourths of a mile distant from the lake shore and then
extending southward through a swamp and valley, are extens-
ive outcrops of quartzless porphyry. This rock extends nearly
to Snowbank lake, on the west shore of which is also a ridge
of schists and conglomerates.

The accompanying section, Plate VI, Fig. 2, (facing p. 160),
from the N. E.4 of N. W. + of sec. 35, T. 64-9, on Snowbank lake,
N. W. tothe of S. W. fof sec. 22, on Moose lake, fairly repre-
sents the rocks north of Snowbank lake. The direction is nearly
northwest and southeast, directly across the strike of the verti-
cal formations. Beginning at Moose lake the numbers corres-
ponding to those on the diagram denote the different kinds of
rocks occuring along this section.

1. Sericitic schist. At the lake shore this schist is dark in
color, fine grained and has a greasy appearance. One hundred
and fifty paces from the shore at the base of a perpendicular
cliff one hundred feet high is a light colored sericitic schist
(165E) with small angular and round feldspars.

2. At the top of the cliff this rock grades into a schist
(164), in which the feldspar nodules have developed to well
defined knots one-fourth of an inch in diameter. The schists
stand nearly vertical, dipping at different places slightly to
the north or south. The strike is ‘about northeast and south-
west, although in some places along Moose lake it varies
from east and west to nearly north and south. Two hundred
paces from the top of the cliff the rock has changed to a dark
argillitic, sericitic schist (166E), in which the knotted structure
has been dveloped to a greater extent. From the same out-

152 TWENTY-SECOND ANNUAL REPORT

crop specimen 167E shows feldspars two inches long. The
weathered surface here looks somewhat similar to that of the
finely. concretionary greenstone of Ely.

3. ‘Two hundred and fifty paces farther and on the south
side of a small swamp, is an extensive outcrop of argillyte
(277). This rock breaks up into small chips and tablets an
inch thick.

4. Two hundred paces from the last outcrop, in a dense
balsam thicket, is a knob of conglomerate fifty feet in diam-
eter. In the conglomerate are numerous rounded and angular ~
pebbles of jasper, varying in size from very fine grains to those
three inches in diameter. Many of these pebbles show beau-
tiful banding. Besides this jasper are gneiss, granite and slate
pebbles not exceeding four inches in diameter. The matrix of
the conglomerate is fine grained and green in appearance
(276E). In another outcrop of this conglomerate fifty paces
northeast of here granite boulders a foot in diameter are com-
mon. The conglomerate forms the highest part of the ridge
south of Moose lake.

5. In the next one hundred paces there is descent of
seventy-five feet intoa swamp about amile wide. Near the
northern edge of the swamp is an outcrop of quartzless por-
phyry, which cuts the conglomerate and forms mica schist as a.
contact rock. In crossing the swamp there are occasional
outcrops of porphyry.

6. In the N. W. fof S. W.+iof sec. 26, T.-64-9, about two
hundred paces west of Snowbank lake, the porphyry cuts a
bed of conglomerate. This differs from number 4 in that no
jasper pebbles were fotmnd.

7. In the conglomerate are beds of epidote schist, and the
whole grades into argillyte. No distinct boundary between
this bed and the preceding one can be marked out.

8. About four hundred paces southeast of number 6 and on
the broad point in section 26 the argillyte grades into a horn-
blend mica schist which is considerably contorted and cut by a
hornblende granite.

9. The granite continues to the shore of Snowbank lake in
the N. W. 4 sec. 35, T. 64-9.

Of this series of rocks the porphyry is the most important.
Quartz porphyry dikes are of common occurrence in the
Keewatin rocks of Minnesota, but in no place does it occur in
such a large mass as it does west of Snowbank lake. Here it.

STATE GEOLOGIST. 153:

extends in a northeast and southwest direction from the center
of section 23, T. 64-9, through sections 27, 33 and 34, then west-
ward to the west range line of T. 64-9, a length of five and one
half miles; it varies in width from three fourths to one and one
half miles. The rock is exceedingly hard, but owing to the
basaltic structure, it readily breaks into angular blocks. The
area in which this prophyry occurs is covered with these
blocks. The readiness with which the prophyry breaks into
angular blocks probably explains why it is found in a valley
between ridges of mainly sedimentary rocks. Although these
latter rocks are more easily abraded by the ice and at present
decompose more rapidly, the porphyry being easily broken
off in large blocks would be removed in much larger amounts
leaving a depression between the clastics. When freshly
broken the porphyry has a purple to grayish color. Ona
weathered surface the rock is white and occasionally is stained
yellow or red by ferric oxide. Porphyritic crystals of felds-
par are numerous; those of quartz are rare and in the larger
number of specimens are entirely absent. Under the micros-
cope felspar phenocrysts of all sizes, up to one fourth of an
inch in length, are embedded in a microcrystalline groundmass
of quartz and feldspar. The feldspars are orthoclase and
oligoclase and show a more or less altered condition. In 60E
the feldspar has been replaced by quartz. Quartz phenocrysts
occur only in small quantities and sometimes are pseudo-
morphs after the feldspar. Chlorite and epidote occur in small
flakes throughout the rock. Biotite and apatite are rarely
present. Specimen 49aH# represents the quartzose phase of
the porphyry. In thin section, besides the usual constituents,
there are numerous quartz phenocrysts. These, with but one
or two exceptions, occur as round grains with corroded edges,
and have a wavy extinction. The felspars are exceptionally
well developed. Epidote is present in small plates and
chlorite is scattered throughout the section.

Whenever the relations of the porphyry and the other rocks.
of this region could be determined it was found that the
porphyry cuts the Keewatin rocks, sending dikes far across
the strike of this formation. A great deal of the disturbance
of the Keewatin rocks in this locality is due to the intrusion of
the porphyry and not, as it is generally supposed, to the
granite of Snowbank lake, which is the youngest formation in
region. Dikes of granite (56E) cut the green schist (58E) and

154 TWENTY-SECOND ANNUAL REPORT

the porphyry (55E) in the S. E. + of the N. W. + of sec. 26, T.
64-9. This is the only place known where the relations be-
tween the granite and the porphyry could be determined with
certainty. The general strike of Keewatin sedimentaries is
parallel to the periphery of the porphyry mass. On the west
shore of Snowbank lake this strike is somewhat modified by
the granite intrusion.

In going from the bay in Snowbank lake in the N. W. i of
S. E. 4 sec. 24, T. 64-9, north 20° west to Newfound lake, the
following outcrops of rocks were seen in the order given:

1. Mica schist and conglomerate in inseparable beds; the
former becoming less schistose and micaceous as the distance
from the granite area increases.

2. Argillyte.

3. Mica schist.

4. Coarse diabase.

5. Agglomeratic greenstone.

6. Conglomerate.

7. Argillyte.

8. Diabase similar to number 4.

9. Conglomerate and argillyte.

10. Sericite schist at three-fourths of a mile from Snow-
bank lake. This schist continues to Newfound lake.

The strike of the rocks mentioned above is nearly east and
west, and toward the east this remains the same. One-half a
mile west of the line of the cross section the strike of the rock,
is somewhat changed to a southwest and northeast direction.
Farther west, near the north end of Moose lake, the strike, as
previously mentioned, is nearly north and south.

In the region north of the central part of Snowbank lake no
outcrops of the porphyry, which is so abundant west of here,
were found. On the west shore of Boot lake, in the S. W. + of
N. W. + sec. 21, T. 64-8, are several large dikes of this rock
cutting the graywacke and schist in this vicinity.

In the S. W. + of N. E. 4+ sec. 21, T. 64-8, on the east side of
the long point, in the midst of a bed of conglomerate, is a boss
of granite partially uncovered. Dikes run out from this mass
in all directions, cutting the conglomerate and distorting the
strata in a very complicated manner. In the conglomerate are
boulders up to four feet in diameter of gneiss, slate, diabase
and granite. This last can scarcely be distinguished from the
granite which cuts the conglomerate of the region. In several

STATE GEOLOGIST. 155

instances a granite dike traced several hundred feet was
found to cut some of the large boulders in the conglomerate.
The contact between the dike and the granite boulders could
not be determined easily. Parts of the boulders adhered to
each side of the dike.

The granites.

The granites of Snowbank lake present an interesting prob-
lem, as there is some evidence to show that two distinct
granites exist here,—an augite and a hornblende granite. The
field evidence at hand is not sufficient to warrant an assign-
ment of any definite relations to these granites. The northern
shore of the lake is made up of schists and argillytes with sev-
eral small areas of granite occurring as dikes cutting the other
rocks and on the extremities of some of the points projecting
into the lake.

On the west side of the narrow bay in the W. + of sec. 20, T.
64-8, is a large outcrop of a light gray granite (271E). The
rock is medium grained and the ferro-magnesian minerals con-
stitute about one-half of the rock mass. Under the microscope
this rock is shown to be an augite granite. Orthoclase, micro-
cline and oligoclase occur in equal proportions. All of the
feldspars have a well defined clear zone around a kaolinized
center and are in some cases prophyritically developed. Quartz
is not very abundant and occurs in small grains. The augite
and hornblende are closely associated. The augite is of a light
green color, has no pleochroism and extinguishes from 45° to
50°. It forms the cores of the hornblende which has a darker
color, is pleochroic in brown and dark green and extinguishes
at less than 22°. The cleavage of the hornblende is a continu-
ation of that in the augite core. The line of division between
the two minerals is distinct and the extinction angle of both
minerals is readily measured along the same cleavage. One
pyroxene plate is unaltered, and its extinction and striations
bring it near to diallage. Hornblende occurs in several places
in bent bundles of slender rods. Sphene occurs in double
wedges and rounded grains. Magnetite and biotite are second-
ary and are not abundant.

Near the section line between sections 19 and 20 this rock
(271E) is cut by a granite porphyry (270E). The speci-
men shows the porphyritic condition of the rock, which,
as a whole, has a more even texture. In thin sections
are found regular phenocrysts of orthoclase and oligoclase

156 TWENTY-SECOND ANNUAL REPORT

embedded in a microcrystalline groundmass of quartz, feldspar
and ferro-magnesian minerals. This rock also cuts and has
greatly modified the schists and argillyte. As these horn-
blende and mica schists grade into the argillaceous slates and
graywacke and have their most perfect developement at the con-
tact with the granite, their highly crystalline condition is due
to the action of the granite upon the other rocks.

On the east side of the bay mentioned above hornblende
granite cuts the older rocks (273E). It has a medium texture
and under the microscope shows the feldspars, quartz, horn-
blende, biotite and a yellow decomposition product, which
stains the feldspars and is most likely limonite.

Since the discovery of augite in the granite from Snowbank
lake the writer has, so far as time would permit, examined
specimens collected by the survey. The following specimens
are from this locality.

Specimen 521G*, from the S. E. 4 of N. E. } sec. 24, T. 64-9,
is a fine dark hornblende granite. Under the microscope this
shows the feldspars, hornblende, sphene and magnetite. The
hornblende has altered to chlorite and shows no traces of
augite.

522G, from the island in the N. E} of S. W. 4 sec. 19, T. 64-8,
is an augite granite. The mineral constituents are the same
as in 271E. Augite and hornblende are present in separate
plates. There is no direct alteration of the former into the
latter, but the hornblende possesses the fibrous cleavage of
uralite and is a paramorph after the augite. Biotite is second-
ary from the hornblende. In this section we have a change of
augite to hornblende, which in turn is altering to biotite and
chlorite.

523G, from the N. W. } of 8S. W. 4 sec. 29, T. 64-8, 1s a
medium grained hornblende granite of a light gray color. Ex-
amined in thin section, this rock shows the usual composition
of the hornblende granite in this locality. The feldspars are
considerably altered, quartz occurs only in small grains, and
the hornblende is highly pleochroic in green and brown.
Sphene is the oldest mineral. Magnetite is largely secondary.
Limonite, an alteration product, stains the rock yellow. Com-
bined with the kaolin of the feldspar this produces a yellow
powder which is easily removed from the rock and leaves cay-
ities. In the hand specimen this peculiar yellow stain is very
noticeable.

*U. S. Grant, 20th Annual Report, pp. 66-67.

STATE GEOLOGIST. 157

524G, from the east shore of the large island (Boot island) on
the range line between T. 64-8 and 64-9, is a coarse augite
granite. In general the rock is the same as 271H, differing
only in the character of the augite, which in this section is
fresh, shows no signs of alteration, is not pleochroic, extin-
guishes at 45° and has a deep green color.

1722 N. H. W., from the island in S. W. 4+ of S. W. 4 sec. 380,
T. 64-8, is a very fine grained granite with orthoclase, micro-
cline and quartz phenocrysts in a microcrystalline base of
quartz and feldspar. Hornblende occurs in small scattering
plates and is greatly altered. Sphene, magnetite and limonite
complete the mineral constituents.

From the above descriptions it is evident that this augite
granite occurs at a number of places around Snowbank lake,
and an examination of specimens from different outcrops in this
locality will probably show 2 wider distribution of this rock.

Without going into the details of the field observations re-
corded in the 15th, 17th and 20th annual reports, it will be
sufficient to say that all geologist have described two granites
hitherto designated in the field as red and gray syenites. The
former and of these is a hornblende granite and the latter an
augite granite. The exact relations of these granites to each
other and of the gray granite to the sedimentaries of this re-
gion are still doubtful. The gray granite has not been found
in contact with the schists, argillytes and conglomerates of
the region, and it is cut by the red granite which also cuts
the schists. The most reasonable explanation which can at
present be assigned to the occurence of these granites in the
same area, is that they are parts of the same magma and that
the tornblendic variety was erupted at a later dated and per-
haps at a time of greater violence than that of the eruption
of the augite granite, which formed the outer portion of the
magma. As there is sufficient reason to place all of the erup-
tive pre-Animikie granites of Minnesota into one period, in com-
paring this area with the other granite areas the following
facts must be considered: on Kekequabic lake the augite gran-
ite cuts the Keewatin sedimentaries;* in the White Iron lake
area the dark hornblende granite, which corresponds to the
augite granite, has the same relations to the Keewatin, as that
in the preceding instance; in all localities where the light col-

*U.S. Grant, 2ist Ann. Rep., p. 38.

158 TWENTY-SECOND ANNUAL REPORT

ored granite is found, it is the later granite and has caused a
greater. disturbance than the augite granite; and wherever
granite pebbles and boulders are found in the Keewatin con-
glomerate, they are almost wholly made up of light colored
granite similar to that which cuts these older rocks. The last
ase is well illustrated by the granite on Boot lake, described
ona preceding page.

Augite granite has been found only in two localities in north-
eastern Minnesota, viz., Snowbank and Kekequabic lake areas.
In the granite specimens collected and described by Dr. Alex.
Winchell as augite granite from White Iron and Saganaga
lakes, a microscopical examination fails to show augite. The
mineral taken as such is only hornblende, which occurs in dark
masses varying in size from the lenticular patches a few inches
in diameter to the irregular areas a fourth of a mile in length.
A microscopical examination of a number of thin sections sec-
tions from these peculiar areas shows that the rock is com-
posed of hornblende, occasionally some feldspar and rarely
quartz. Biotite is due to the alteration of the hornblende. |
The sagenite structure of rutile is well shown in several slides.

In central Minnesota* the occurrence of the dark inclusions
in the granite is the same as that of those just mentioned in
the northeastern part of the state. The mineral composition,
however, is somewhat different. In thin section these are
found to consist of fresh augite or hornblende, with all degrees
of alteration of the former to the latter, showing conclusively
the secondary origin of the hornblende. Other evidence also
shows that most of the hornblende granite of the same locality
was originally an augite granite.

From the foregoing notes it is seen that the granite forma-
tion of Minnesota, which finds its greatest extent in the moun-
tain masses of the Giant’s range, although in the larger part
of its area a hornblende granite, yet in other parts there are
unmistakable proofs that it was originally an augite granite.

The present altered mineralogical composition of the granite
is accounted for by the explanation suggested by Prof. N. H.
Winchell to explain the great strength of Minnesota granites:t+
‘‘We may perhaps account for the greater strength of Minne-
sota crystalline rocks by supposing them less changed super-
ficially by the process of decay, the lateness of the glaciation

*For information concerning this locality the writer is indebted to Prof. C. W. Hall.

+N. H. Winchell. ‘The comparative strength of Minnesota and New England
granites.” 12th Ann. Report, pp. 14-18.

STATE GEOLOGIST. 159:

to which they have been subjected having left them compara-
tively fresh through the recent removal of a considerable
thickness.” Every one familiar with the occurrence of this
granite formation will recognize the fact, that in the localities
where augite has been found as one of the original constitu -
ents, the glacial action has been more pronounced and has
removed a great thickness of the surface rock, up to that time
undisturbed, leaving a much fresher rock than elsewhere, and
in which one would naturally expect to find a facies of the
formation nearer to its original condition.

In connection with the preceding it may be of interest to
note that the hornblende and mica schists of Snowbank and
White Iron lakes grade into argillaceous slates and conglom-
erates. The schistose character is most fully developed at the
contact with the granite. All evidence tends to show that the
schists are due to the intrusion of the granite and suggests
that the narrow belts of schist generally found between the
granite and the Keewatin rocks and which have hitherto been
designated as a separate formation (Coutchiching or Vermilion)
are only altered portions of the Keewatin which have been
subjected to the heat and action of the intrusive granite.

lll. ACTINOLITE MAGNETITE SCHISTS FROM THE EASTERN
MESABI RANGE.*

The writer while studying the peculiar rock occurring along
the central part of the northern periphery of the great gabbro
belt, designated as the Pewabic quartzyte, found in the vicin-
ity of Birch lake an extensive area of actinolite magnetite
schists associated with the Animikie. The derivation of these
schists from a rock containing a carbonate of iron and their
lithological similarity to those found in the Penokee series
tend to establish an important analogical link between the two
series of which they are a part.

Since this investigation was carried on, actinolite schists
from this locality have been described by Dr. W. S. Bayley.t
These descriptions and the additional evidence obtained during
the summer of 1893 confirm the views previously expressed by
the writer.

*Extract of a thesis accepted for the degree of Master of Science in the University of
Minnesota. Read before the Minnesota Academy of Natural Sciences, May 1, 1893.

+Amer. Jour. Sci., ILI, Vol. xlvi, pp. 176-180, Sept., 1893. The writer wishes to ac-
knowledge the kindness of Dr. Bayley for the opportunity given to examine the
slides used in his descriptions.

160 TWENTY-SECOND ANNUAL REPORT

The accompanying map (Plate VI, Fig. 1,) of the west end
of Birch lake gives a comprehensive view of the geological
structure of this region. The contour lines were taken from
the topographical notes of Mr. A. D. Meeds.

Numerous specimens have been collected hy the state survey
from this locality.* Nearly all these have been examined in
thin section. In the following pages the descriptions of the
occurrences of the field outcrops are taken from the annual
reports of the survey, where more detailed accounts may be
found. Beginning with the western extent of this area, where
the Animikie approaches nearest to its normal condition found
on the western Mesabi, the formation is traced through con-
tinuous outcrops to the north shore of Birch lake, where it
disappears under the gabbro, and where the crystalline char-
acters have the highest development. In studying the variety
and the extremes of the lithological characters, and by noting
the gradual change of one extreme into the other, we have un-
disputable evidence of the origin of the crystalline portions
of the formation. The object of the following paper is to show
the derivation of the actinolite schists and their rela-
tions to their geological associates in the vicinity of Birch lake.
The fact that the so-called ‘‘Pewabic quartzyte,” between
Birch lake and Gunflint, is a part of the iron bearing portion
of the Animikie will also be shown.

Specimens collected by Prof. N. H. Winchell.

The following specimens, collected by Prof. Winchell,+ were
examined in thin sections by the writer. Several diamond
drill sections have been made under the management of Capt.
Wicks. Of these the one (No. 5) on the N. W. 45S. W. 4see. 27,
T. 60-18, gives the most complete rock section as well as that
of the greatest thickness. In ascending order the rock found
here is as follows:

1636. Granite, 3 feet.

1635. Bottom of quartzyte, 1 foot.

1634. 10 feet. A hard siliceous greenish rock, which con-
tains many fragmental grains of quartz. In thin section the
quartz grains appear angular and show no signs of enlarge-
ment. They are derived from the granite, some contain numer.
ous rutile needles and are full of inclusions. The matrix is com-
posed of microcrystalline quartz and aphanitic green material

*H. V. Winchell. 17th Ann. Rept., pp. 81-96.
+21st Ann. Rept., pp. 82-86.

—=—

Geol. and Nat. Hist. Sur. Minn XXII Ann. Rept. Pl. VI.

Ve.
747 Va fe

ease *
2 7a teens

+4+te
t —+—
jt tH 4+ ele tt oF

EF Fl ROR FF
Pa aes gee 5 ey
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GRANITE. =] |Ron-BEARING BEDS. (s“lCassro.

Fic. 1. GEOLOGICAL MAP OF THE WESTERN END OF BIRCH LAKE AND AD-
JOINING COUNTRY SOUTHWARD.

nw s

f <=

& f te

z 4 oo

al (

2
a
Sy
=

Fic. 2. CROSS-SECTION FROM MOOSE LAKE TO SNOWBANK LAKE. NORTH-
WEST TO SOUTHEAST. DISTANCE TWO MILES. ALTITUDES EX-
PRESSED IN FEET ABOVE THE SEA-LEVEL.

STATE GEOLOGIST. 161

which has a tendency to form actinolite needles. These needles
occur in bundles and in some cases penetrate the quartz grains.
The transition upward to the next is gradual.

1633. 15 feet. Round fragmental quartz grains cemented
in a matrix of quartz. In thin section this shows rounded frag-
mental grains of quartz embedded in a microcrystalline matrix
of quartz and some green material. Some of the quartz grains
show a slight enlargement, being bordered by a ragged rim of
fine grained quartz with similar orientation.

1632. 17 feet. Fine grained pinkish-cream colored quartz-
yte. The hand specimen is composed of microcrystalline silica
similar to the matrix of the preceding section.

1631. 24 feet. Siliceous, fine magnetite. On account of the
high percentage of red hematite and magnetite this rock in
thin section is nearly opaque. A few small grains of quartz
were seen.

1630. 20 feet. Gray quartzyte, nearly all silica with round
concretions. This isa magnetitic concretionary chert. Rough-
ly oval and rhombic outlined areas of magnetite and hematite
occur in a cherty background. The magnetite occurs in small
cubes and the hematite is distinguishable only in reflected light
by its red color. ‘These two minerals occur in alternating
bands in the same concretions. The iron oxides are often
concentrated upon the exterior of the areas, and in some cases
they have grown beyond the outer borders and extend into the
cherty background.*

Another section from the same specimen shows a concre-
tionary actinolitic chert. The concretionary structure is not
so marked as in the preceding section. A considerable amount
of a greenish mineral matter is present. Under a high power
this shows the development of fine actinolite needles and plates.

1629. 70 feet. ‘‘Black slate” heavily charged with mag-
netite. Magnetite occurs in well developed crystals and com-
poses nearly the whole section. Well developed plates of
actinolite lie between the grains of magnetite.

1628. 157 feet. Black and gray, fine banded rock, with fine
grained magnetite, the latter being distributed through the
whole, and sometimes concentrated along planes of weakness
in beds six to ten inches in thickness. The banding is wavy.
A thin section of the drill core cuts the light and dark bands of
the rock. The light colored bands are composed largely of

*Compare; R. D. Irving and C.R. Van Hise. 10th Ann. Rep. U.§. Geol. Survey, p. 490.

162 TWENTY-SECOND ANNUAL REPORT

greenish aphanitic material showing numerous minute crystals
of actinolite. Other portions of these bands have large plates
of actinolite. The magnetite is concentrated along certain
lines and extends into the actinolite bands. In places it ap-
pears in aroughly concretionary form. The actinolite in this
section has been developed to a greater extent than that in the
rock lower down in the series. :

The above drill section represents a total thickness of three
hundred and twenty-one feet. A number of other drills have
been made in the same region. The succession of the different
rocks is the same as that described above. The different strata
vary in thickness as the extreme northern edge of the forma-
tion is approached. The only rock of uncertain thickness is
number 1632, the fine grained pink quartzyte, which is absent in
some places. The whole of the quartzyte is wanting a short
distance east of this locality. A drill hole sunk in section 13,
T. 60-13, passed through one hundred and ninety feet of hard
‘jaspery taconyte’ banded with ore and resting upon the
granite. The bands of ore were five or six inches thick, and
the iron ore was hard, black and nearly always magnetic.

Specimens collected by H. V. Winchell.

In describing these specimens, they will be taken up in the
order of their occurrence from the west toward Birch lake.
Detailed notes of their occurrence may be found in the 17th
annual report, and page references refer to this report and
the numbers refer to the specimens.

373. (P. 86.) S. W. tofS. W. 4 sec. 32, T. 60-13. This is
a black slate, and is composed of a clouded aphanitic mass of
brownish material, which shows some clear pieces of actinolite.
Magnetite is not very abundant.

369. (P. 85.) Iron lake, N. H. } sec. 23, T. 60-13. A black
magnetic rock lying nearly horizontal. The magnetite and sid-
erite occur in well defined crystals. Part of the latter in thin
plates is translucent. The green aphanitic mass of the rock
has developed into plates of actinolite.

365. (P. 84.) N. W. 4 sec. 24, T. 60-13. In a perpendicu-
lar wall eight feet high and several rods long of a heavy black
rock. This is a concretionary actinolite slate, composed of
aphanitic green material considerable developed to actinolite.
Actinolite forms small oblong concretions, in which the fibers
have a radial structure similar to that of the mineral in the
zeolites. Needles and prisims of the amphibole penetrate and

STATE GEOLOGIST. 163

cross these concretions. Magnitite is confined to the concre-
tions.

364. (P. 83.) Is aconglomerate boulder.

363. (P. 83.) ‘A smoothed, black exposure of ferruginous
quartzyte several acres in extent appears on the surface of the
ground in the N. W.4 of N. E. } sec. 19, 60-12.” The rock
and magnetite both weather shiny black. The specimen is
largely composed of magnetite which occurs in concentrated
parallel bands. Actinolite forms the light colored bands of
the rock. Itis present in small fresh prismatic plates 2 mm.
in diameter.

362. (P. 82.) Near the last locality. Banded magnetite.
This consists of several alternating light and dark bands. The
latter are due to the concentration of magnetite which gradu-
ally decreases in quantity as the borders of the light bands are
reached, and in the interior of these bands it occurs only in
isolated grains. The light bands are composed of almost col-
orless grains of amphibole, the characters of which cannot be
determined. This section represents an intermediate stage of
developement between the slates composed of aphanitic and
unindividualized green material and the actinolite magnetite
schists represented by Dr. Bayley’s specimen No. 8783.

361 and 360. (P. 82.) Inthe N. E. corner of sec. 19, T. 60-
12,is a shaft about ten feet deep in a greenish magnetitic slate.
Number 36] is a slate composed of unindividualized matter.
Number 360 is a concretionary amphibole schist. The amphi-
bole occurs in plates and irregular grains, having extinction
angle of 14° to 25°. Actinolite and common hornblende are
both present. Augite occurs in irregular plates, intergrown
with the amphibole. The concretions of the ferro-magnesian
minerals and magnetite lie against a background of medium
grained quartz.

359. (P. 82.) IntheS. W.j ofS. W. 4 sec. 17, T. 60-12, is
@ magnetic quartzyte in strata dipping S. 8S. E. 10° to 12°.
Under the microscope this rock shows the same character-
istics as those of the preceding specimen. The green sub-
stance has not been fully developed to amphibole.

358. (P. 82.) ‘At one-fourth of a mile south of the S. E.
corner of sec. 7, T. 60-12, are numerous angular fragments of
olivinitic magnetite projecting through the moss.” This rock
is largely composed of microcrystalline quartz. The other
constituents are magnetite, hematite and a green substance.
This substance has partially changed to actinolite, forming

164 TWENTY-SECOND ANNUAL REPORT

bundles of innumerable fine needles, some of which penetrate
the quartz. Several rough rhombohedral pieces of a brownish
mineral, probably siderite, are present. An indistinct concre-
tionary structure is also noticeable.

3596. (P. 93.) Iron ore, four hundred paces east of the west
quarter post of sec. 10, T. 60-10.

396. (P. 93.) A short distance south of Birch lake in the
N. E. 4 of sec. 26, T. 61-12, is a knoll of fine grained crystal-
line rock. This is a fine grained gabbro. ‘‘The gabbro ap-
pears in small, detached knobs, lying on the Animikie iron ore
beds. These beds are somewhat disturbed and broken and
vary in dip from 12° to 30° to the southeast. Near these
knolls of gabbro the iron ore rock is semi-crystalline, contain-
ing porphyritic crystals of hornblende sometimes two and one
half inches long, 397. There are large outcrops of this Anim-
ikie rock here. Sometimes the stratification is not very
evident, but generally it is distinct and well marked, 398.”

397. In thin section this consists of large plates of actino-
lite, pleochroic in light and pale green and extinguishing
nearly parallel. Cross sections of the crystals show the char
acteristic amphibole cleavage. Numerous small grains of
quartz are enclosed by the actinolite, which in several cases
forms around a number of the quartz grains a rim of inward
penetrating needles. A few small pieces of plagioclase also
occur. Magnetite occurs in small crystals in the actinolite.

' 398. The mineral composition of this is the same as the pre-
ceding, having in addition augite and olivine. It is of medium
texture. Quartz occupies about one half of the section.

399. ‘Some of the Animikie is almost all quartz which forms
a coarse granular sandstone on decomposing. EH. + of N. W.4
sec. 85, T. 61-12.” This is composed of interlocking quartz
grains including magnetite and actinolite. The quartz inter-
locks by irregular sutures. The magnetite, which is the old-
est mineral, is often in well marked octahedrons enclosed in
the quartz, but more frequently it is in rounded grains, either
surrounded by a quartz individual or situated between several
of them. The actinolite holds the same relation to the quartz
as does the magnetite. Both of these are somewhat altered to
limonite and chlorite. In its present condition nothing re-
mains to show a clastic origin. This character of the rock is
common in the iron bearing member of the Animikie both on
the Mesabi and on the Penokee ranges. It is largely on ac-
count of the abundance of this quartz in the so-called ‘‘Pewa-

STATE GEOLOGIST. 165

bic quartzyte” between Birch and Akeley lakes that this part
of the iron bearing member has been perhaps wrongfully re-
ferred to the basal quartzyte of the Animikie.

401. (P. 94). “In theS. E. $ N. E. }$ sec. 35, T. 61-12, are
several ridges of magnetic quartzyte having vertical faces 15
feet high on the west. A few feet west of one of these walls
of rock there is a knoll of syenite. The quartzyte is in beds
which are nearly horizontal and seem to have about the same
texture and composition where it lies on top of the syenite as
they have ten feet higher up, 401.” This is strikingly similar
to the preceding rock specimen. It is composed of large
irregular interlocking quartz grains, hematite and magnetite,
which shows the original concretionary form so common in the
Animikie slate. A peculiarity in which it differs slightly from
these other slates is, instead of a background of microcrystal-
line quartz, each of the concretions occurs in a separate grain
of quartz. In some of the concretions the hematite and mag-
netite have a banded structure similar to that seen in jasper.
A brown decomposition product, probably limonite, results
from the decay of the iron oxides. The magnetite which does
not occur as round concretions is arranged in bands through
the rock.

402. (P. 95)... “In the N. HE. 4'of S. W. 4 sec. 35, T. 61-12,
the magnetitic quartzyte seems to have been affected by some
metamorphosing agent which has produced large crystals of
hornblende in it.” This is an actinolite magnetite schist. The
actinolite occurs in plates and needles, which extinguish nearly
parallel. The magnetite is irregularly scattered throughout
the whole section. Quartz composes about one-third of the
rock.

404. (P. 95). ‘‘Toward the S. W. 4 of sec. 35, T. 61-12, the
land rises until it is 200 feet above Birch lake. On this high
land many large, smooth-topped exposures are produced by
windfalls. The strataseem to have been disturbed and slightly
elevated by some force from beneath. The usual dip—less than
30° to the southeast—is, however, still maintained. Some of
the beds of this Animikie rock are but slightly iron bearing and
are almost wholly composed of olivine, 404.” A section of this
rock is composed of two-thirds of quartz and the remainder of
actinolite, olivine and magnetite. The quartz occurs in inter-
locking grains as described above. The other minerals occur
as rounded grains within quartz grains or in masses between
the grains. Innumerable fine tufts of actinolite needles pene-

166 TWENTY-SECOND ANNUAL REPORT

trate the quartz grains in all directions. Numerous crystallites
of the same mineral crowd the quartz, forming by their combi-
nation beautiful figures. A yellow decomposition product fills
up the fractures in the quartz.

405. (P. 95). In the N. 3 of the S. E. 4 sec. 24, T. 61-12, the
general occurrence of the Animikie is the same as that south of
Birch lake. Thin strata of rich magnetite are separated from
each other by beds of poor ore or quartzyte, 405. Under the
microscope this rock is found to be made up of quartz, actinolite
and magnetite. The quartz occurs in rounded grains surrounded
by the other minerals, and in irregular interlocking grains,
The actinolite occurs in long slender plates and in bundles of
needles. ‘‘ There is a heavy covering of drift sand and boulders
here. Granite in place and gabbro lying on it were seen a
short distance farther east in the S. E.4 N. W. i sec. 24, T.
61-12. The Animikie beds seen in the vicinity were in knolls
that rise above the granite and gabbro and are estimated to be
150 feet above Birch lake. A thickness of about 25 feet of the
iron-bearing strata was seen in the various shafts.”

The outcrops just noted mark the eastermost extension of
the Mesabi iron-bearing strata, which in the field have been
found to be continuous and of the same formation, although
varying greatly in lithological characters. Farther east are
other isolated outcrops of this formation which will be men-
tioned below.

Other observations.

Other observations have been made in this vicinity by Prof.
Winchell* and the writer.

In the S. E. + of S. E. + sec. 23, T. 61-12, a number of shafts
have recently been made by the Spellman Mining Co., under
the direction of Mr. W. L. Honnold. The largest shaft was
sunk about 200 feet east of the granite. This passes through
black slates, gabbro, iron ore and actinolite schist.

The following notes were. given to the writer by Mr.
Honnold: ‘‘The deepest shaft was sunk 37 feet deep,—7 feet
surface, 20 feet magnetic ore and 10 feet hornblendic quartzyte
(foot wall). Between the ore and foot wall is a seam three or
four inches thick of chloritic material, very soft and probably
resulting from the decomposition of the foot wall. The foot
wall carries considerable ore in irregular distribution, and the
ore passed through at first was apparently due to an unusual
concentration of this. The ‘black slates’ were not encountered

*Twenty-first Ann. Rept., p. 156.

_ STATE GEOLOGIST. 167

in the shaft, but are to be found near the surface about 300
paces east of this shaft. Whether these are a continuous for-
mation or merely a local variation of the quartzyte is undeter-
mined.”

The so called black slates of this locality were found by the
writer only in large blocks removed from their original posi-
tion. They are the same as the black slates south of Birch
lake, but as they are not found in situ north of the lake, they
may be dismissed without further mention. All of the speci-
mens obtains from this vicinity were examined in thin sections
with the following results: The rock called the hanging wall
in the largest shaft is a biotite gabbro of medium texture and
considerably altered. This occurs as detached knobs resting
upon the iron-bearing rock beneath it, in the same manner as
the gabbro south of the lake. The magnetic ore is composed
of a high percentage of magnetite, occuring in well defined
cubes and rounded grains. The interstices between the grains
are filled with plagioclase, augite, biotite and quartz, all of
which are very fresh. The rock associated with the ore is
composed of actinolite. This mineral occurs in large plates
and bundles of numerous beautifully twined crystals. In places
biotite and chlorite show the alteration of the actinolite. A
few grains of quartz are scattered throughout the section. The
‘‘hornblendic quartzyte” is afresh actinolite schist. The ac-
tinolite occurs in crystals several inches in length and encloses
numerous quartz grains. This rock is the same in character
as specimen 960 and described as an olivinitic quartzyte.* In
thin section this rock is an actinolite schist similar to the schist
south of Birch lake. The characters of the minerals in this
section in every way correspond to those shown in Dr. Bayley’s
specimen No. 8783, from which it differs only in coarseness of
texture. In this locality we have, thus, the actinolite schist
and the magnetic ore occurring in alternating bands of great
thickness. The original character of the rock has been totally
obliterated and in its present condition the rock is wholly
crystalline, representing one extreme of the variations in the
lithological character of the Animikie schists.

Specimens collected by Mr. A. D. Meeds in 1893 are nearly
all from the southern limit of the Animikie rocks.

Number 2, is a fine grained gabbro, from the N. W. fof N. W.
$+ sec. 2, T. 60-12.

" *N. H. Winchell, 15th Ann. Rept., p. 335,
+See list of rocks collected by A. D. Meeds, pp. 87-89 of this report.

168 TWENTY-SECOND ANNUAL REPORT

Number 2a, from an outcrop a short distance north of the N.
W. corner of section 2, is the same as specimen 404. described
above.

No. 5, is coarse gabbro, near the east quarter post of sec. 28,
T. 61-12.

No. 6, from the N. E.4 of S. W. 4 sec. 10, T. 60-12, is a fine
grained gabbro.

No. 7, from near the east quarter post of sec. 17, T. 60-12, is
the same as the actinolite schists described above.

No. 8, one-fourth of a mile south of the N. E. corner of sec.
35, T. 60-13, is a fine grained biotite schist. This is a part of
the Animikie slate and is composed of quartz and biotite.

South of this locality the coarse gabbro occurs in numerous
knobs and ridges. Onaccount of the level topography in this
vicinity the contact of the slate and gabbro was concealed by
swamps.

Summary.

In the preceding notes attention is called to the varying lith-
ological characters of the formation under consideration. This
formation has been traced by continuous outcrops from the
Mesabi iron bearing rock to Birch lake. At the western end
the sedimentary character is undisputed. Going eastward the
Animikie gradually thins out until it is lost altogether under
the gabbro. The lithological characters also change, the
nearer the gabbro is approached the more crystalline is the
nature of the rock, until on both sides of Birch lake it is wholly
crystalline. Near the contact with the gabbro, augite and
olivine occur intimately associated with the actinolite and mag-
netite of the Animikie schists. The black slates have been
changed to a quartz biotite schist in the proximity of the
gabbro.

The lithological characters of the actinolite schists may be
divided into two divisions: 1st. Those which are constant
throughout the whole formation: banded structure, due to the
concentration of the iron oxides along lines of weakness, leav-
ing bands of lighter material, which finally makes up the ferro-
magnesian minerals; abundance of secondary quartz; coucre-
tionary structure of the iron oxides, and the presence of actin-
olite, although often in very small amounts. These character-
istics agree very closely with those given by Irving and Van
Hise* for the corresponding formations in the Penokee series.

*10th Ann. Rep. U.S. Geol. Survey, pp. 389-393.

STATE GEOLOGIST. 169

The second division of the lithological characters is peculiar
to the Mesabi formation, as they are largely due to the effect
of the gabbro at the time of intrusion. 2d. Those characters
which vary: mineralogical composition of the alternating
bands. In the western part of the area, the light bands are
composed of an unindividualized greenish substance, and the
dark bands are composed of magnetite and hematite in about
equal proportions, with some iron carbonate. Going eastward
the rock passes through consecutive gradations until the light
bands are made up of actinolite with local variations, where
augite and olivine occur, and in the dark bands the hematite
and siderite disappear, leaving only the magnetite. Plagioclase
has been noted in several instances. SBiotite results from the
alteration of the actinolite.

The Pewabic quartzyte at the bottom of the Animikie
decreases in thickness as Birch lake is approached from the
west, and in the vicinity of Iron lake, section 14, T. 60-13, it
disappears entirely. From this locality eastward the iron-
bearing rock rests upon the granite, and consequently forms
the bottom of the Animikie. The black slates also disappear
before the Dunka river is reached. They were removed at the
time of the gabbro intrusion.

The outcrops of the Animikie below and inclosed by the
gabbro, between Birch lake and Akeley lake, have the same
lithological characters and composition as the actinolite schists
at Birch lake. These scattered outcrops have heretofore been
called a part of the Pewabic quartzyte, but for reasons given
above the writer considers them a part of the iron-bearing strata
of the Animikie*.

IV. THE GABBRO.

Considerable time was spent in making a close study of the
gabbro belt, through its entire width in Lake county. It is in-
tended, on account of lack of time at present, to mention only
a few of the localities where interesting observations were
made.

In townships 62-10 and 11, and 61-10 and 11, an area about
two townships in extent, of a dark, heavy and bedded olivine
gabbro was found. Within this area are numerous knobs of
feldspar rock as clear, fresh and coarse as the anorthosyte
masses found near the lake Superior coast. In many instances
*Nore.—W. 8. Bayley.in the Nineteenth Ann. Rept., pp. 193-210, in describing rocks

from the Akeley lake region, includes much of the so-called Pewabic quartzyte in the
gabbro formation.

170 TWENTY-SECOND ANNUAL REPORT

the feldspar knobs appear like water-worn boulders enclosed
in the overlying olivine gabbro. On Greenwood lake (T. 58-10)
are extensive outcrops of fresh hypersthene gabbro. This is
cut in several places by dikes of the red rock which forms
Greenwood mountain south of the lake. <A point of importance
in studying the gabbro is that the gabbro along the center of
the formation has a beit in which are numerous knobs and
areas a mile in extent composed of plagioclase rock, similar to
that mentioned above. In going from the northern and south-
ern limit of the gabbro toward this belt, it is very noticeable
that the ferro-magnesian minerals decrease and the feldspar
increases in proportion. The rock has more of a stratified ap-
pearance arising from the arrangement of the constituent min-
erals in bands. This separation of the minerals, when carried
to extremes, produces the large aggregations of feldspar. The

coarseness in texture is affected in the same manner. In the —

gabbro we have every evidence that it was a batholitic intrus-
ion rather than a surface flow. The mineral and chemical com-
position of the various parts of the formation conform to all
the known rules which govern the cooling of liquid magmas.

V. THE RED ROCK.

Under this group are included the felsytes, some of the dia-
bases, and the augite syenite, which are closely associated and
form a prominent group. The following are descriptions of all
the outcrops examined by the writer, within the boundary of
this group, as indicated on the map (Plate V, p. 150). In the N.
E. + of the S. W.4 sec. 8, T. 57-7, is the most northern outcrop
of the dark diabases of the lake Superior coast. One half of
a mile northwest of this, on the slope of a high ridge, are
numerous angular fragments of augite syenite. At the top of
the slope, rising four hundred feet in three fourths of a mile, is
a perpendicular wall of fiery red augite syenite (225 HE), sim-

ilar to that found on the slope. The land continues at about

the same hight north from here, and is covered with swamps.
The rock is exposed in scattering outcrops and is the same as
number 225E. Microscopical examination shows that this
rock is the same as that described from Eagle mountain*. No
augite was found in the section. Chlorite is present in small
flakes. There are numerous patches ofa yellow decomposition
product which is easily removed, leaving a kind of porous

*R. D. Irving. Copper Bearing Rocks, Monograph V, U.S. G.S., p. 124, figs. 1 and 2,
plate XIV.

STATE GEOLOGIST. f/f

structure: Quartz has thoroughly saturated the rock, and some
of the cavities just mentioned are partially filled with quartz
crystals, showing the progress of the saturation. The only
original minerals definitely determm®med are orthoclase and
oligoclase.

Seven miles north of the last outcrop, at the north quar-
ter post of sec. 31, T. 59-7, is a large outcrop of felsyte
porphyry, 172E. The weathered surface shows flowage struc-
ture on a large scale, 173H. Large black segregations show
the peculiar bent and contorted condition noticed in the felsytes
near lake Superior. In the N. W. 4 of N. W. 4 sec. 31, T. 59-7,
are numerous angular fragments of laminated felsyte, 174E.
This rock was not seen in place, but occurs in the outcrop one-
half a mile east of here.

The next outcrop north of here is in the N. W. j of sec. 36,
T. 60-8. In the valley at this place is an exposure of black
fine grained diabase nearly one half of a mile wide. The rock
has a basaltic structure and in many places it is crossed by fine
veins of quartz, 171E. Under the microscope the section shows
long lath-shaped plagioclase, augite and magnetite. All of
these are considerably altered. In portions of the section are
porphyritic crystals of plagioclase. This rock is similar to the
diabase cutting the felsytes north of lake Superior. It was not
found in connection with the felsyte and augite syenite in this
locality, but since in other localities it is always associated with
these rocks it is safe to assume that it marks the northern edge
of the red rock group in T. 60-8.

On Greenwood lake the gabbro is cut by dikes of augite
Syenite varying in width from one inch to two feet, 180E. This
is the same as the rock which occurs in extensive outcrops
south of the lake. Greenwood mountain is a mass of fiery red
augite syenite, 185K and 186E. The rock is of medium texture,
consisting mainly of feldspar and quartz. In ordinary light a
section of this rock shows a red stained field completely riddled
by secondary quartz. The quartz is wholly secondary and in
many cases assumes a graphic form. The feldspar is mostly
orthoclase with some oligoclase. These minerals have been
corroded, broken up and replaced by infiltrating quartz. All
of the quartz grains in any feldspar crystal are similarly
oriented and in no case do those in adjacent feldspars possess
the same orientation.

In the S. E. + of S. E. 4 sec. 1, T. 57-11, on the north side of
the low ridge, are several outcrops of felsyte porphyry, 184E.

172 TWENTY-SECOND ANNUAL REPORT

In microscopical characters it is similar to the following. Near
the Beaver Bay trail in the S. E. } sec. 33, T. 58-10, on the
south side of the broad ridge, are extensive exposures of
felsyte, 181E. ‘‘Large surfaces ‘ten to twenty-five feet’ square
show fluidal structure on a large scale. Pale pinkish, light
green and black felsytes are twisted together in various forms
and assume a banded structure. The contrast between the
colors is very strong. Under the microscope it is apparent
that this rockis a felsyte with a quartz saturated base.”*. The
base is microcrystalline and of a red to purple color; the alter-
nation of the lighter and darker portions gives a wavy band-
ing to the rock. Red porphyritic feldspars are numerous.

A mile southwest of this outcrop and on the south side of
the swamp which covers the region between the two, is an out-
crop of felsyte porphyry, 182EK, N. W. 4 sec. 3, T. 57-10. Mi-
croscopical examination shows numerous orthoclase pheno-
cryts embedded in a red to black aphanitic groundmass. The
feldspar is somewhat altered to kaolin and shows shattering
before the solidification of the base. The felsyte is cut by a
fine grained diabase dike fifty feet wide, 183E. This is the
same as the rock found in sec. 36, T. 60-8. South of these
outcrops no others were observed, until in the S. W. 4 N. W. 4
sec. 4, T. 56-9, where the diabase of the lake Superior coast
is found.

During the spring of 1892 Mr. C. L. Chase of Hastings, Minn.,
while surveying townships 56-9, 10 and 11, collected specimens
from all of the rock outcrops upon the section lines in these
townships. These specimens are registered in the general
museum list and are briefly described as follows:

8026. Diabase from the S. E.18S. E. } sec. 4, T. 56-9. This
is from the same outcrop from which 215E was taken.

8027. Anorthosyte. 1,500 paces north of S. E. corner see.
5, T. 56-11. This is north of the red rock belt.

8028. Diabase. 25 chains west of S. E. corner sec. 2, T.
56-11. This belongs to the diabases south of the red rock.

8029. Felsyte porphyry, S. W. 4S. W. 4sece. 15, T. 56-11.

In the N. E. 4 of N. E. 4 sec. 4, T. 56-11, is a ledge of dark
diabase, thirty feet high, facing northward and sloping
toward the south, No. 8032. A short distance north of here on
the north side of a small stream is alow east and west out-
crop of gabbro, No. 8031. A dike of felsyte porphyry cuts the
gabbro, No. 8033. Farther than this the relations of these

*Irving, op. cit. Description and illustration, p. 38.

STATE GEOLOGIST. 173

rocks were not determined. The dark diabase is the same as
that which was found cutting the felsyte in localities described
above.

On the range line near the northwest corner of sec. 19, T.
55-11, Mr. A. D. Meeds found gabbro and felsyte porphyry in
contact. From this exposure the relations of the rocks could
not be determined. The region generally is covered with drift
and swamp, which conceal all outcrops. One half a mile
south of the last outcrop the felsyte again occurs. This prob-
ably represents the southern limit of the red rock belt in this
locality. The specimens collected show red porphyritic feld-
spars embedded in a dark aphanitic groundmass. The gabbro
is the coarse black phase of the great gabbro formation.

The bedded red rock surface flows of the lake Superior
coast are traced by almost continuous outcrops into the great
body of the red rock. The amygdaloidal and compact dia-
bases cover the so-called fine grained gabbros or diabases
south of the red rock group.

The varying composition of this group has been noted by
other writers. Irving* says: ‘‘These three varieties of red rock
[same as described above] thus described as occurring at Du-
luth, are evidently but different phases of the same rock, and
without much doubt connected with each other in the mass,
though this was not proved in the field.” Although recogniz-
ing the fact that the different varieties of this group were found
cutting all of the subdivisions, Irving places them in the differ-
ent groups somewhat arbitrarily.

To the writer it seems that the Keweenawan on the north
shore of lake Superior can be divided most satisfactorily into
three large groups, with a possible smaller group, which in
chronological order may be called the gabbro, diabase, red rock
and the Jater dikes along the shore.

VI. THE DIABASES.

Under this group are included the fine grained dark gabbros
so called, and the diabases forming Irving’s different groups
of the Keweenawan above the basal gabbro. Placing the amyg-
daloidal diabases and their related rocks in their proper posi-
tion, i. e., into one large group, it is evident that the grouping
of Irving must be readjusted. As a whole. this group is made
up of a diabase porphyryte, which surrounds the anorthosytes.

*Copper Bearing Rocks, p. 272.

174 TWENTY-SECOND ANNUAL REPORT

In the region back of the lake shore it is impossible to sub-
divide the rocks into the different groups of Irving. The
lithological characters vary but little over large areas and
would tend to show the unity of these groups rather than
numerous subdivisions. The continuity of the rock outcrops
in a measure serves to strengthen this view. This is the rock
which transported the anorthosyte to its present position and
represents the effusive portion of the magma, out of which the
basal gabbro first cooled.

VII. THE ANORTHOSYTES OF THE MINNESOTA SHORE OF
LAKE SUPERIOR.*

These rocks are discussed in detail by Dr. A. C. Lawson.t
The first part of that paper takes up the petrographical char-
acters. In the second part the distribution and mode of occur-
rence of the anorthosytes are discussed. These rocks were
observed between Carlton peak and Encampment island, a
distance of forty-six miles, and extend an unknown distance
inland. The occurrence and character is described at the fol-
lowing points on the lake Superior coast: Encampment island,
Split Rock point, Beaver Bay, shore below Beaver Bay, Bap-
tism river, slope of Sawteeth mountains, Carlton peak.

In discussing the geological relations of the anorthosyte, it
is considered as a pre-Keweenawan terrane for the following
reasons: It is traversed by dikes, both acid and basic, of the
Keweenawan eruptives; the Keweenawan lavas hold imbedded
in them innumerable boulders and blocks of anorthosyte evi-
dently detached from a pre-existing terrane; the anorthosyte
forms the surface upon which the Keweenawan lavas now rest
and upon which they were originally extravasated; the anortho-
syte affords both by its petrographical characters and by the
nature of its surface the most satisfactory evidence of profound
erosion prior to the extravasation of the Keweenawan erup-
tives. A great interval must have elapsed during this erosion,
and the recognition of a pre-Keweenawan terrane involves cer-
tain consequences of geological importance. One of these is
the absence of the Animikie in the region of study; another is
the correction of Irving’s estimate of the thickness of the
Keweenawan. Instead of 20,000 feet in thickness, this is
placed at barely 2,000 feet. The anorthosytes are plutonic

*Read before the Minn. Acad. of Nat. Sciences, Dec. 26, 1893.
+Bulletin No. 8, pp. 1-25, 1893.

STATE GEOLOGIST. 175

eruptives, invading the Archean and yet long anterior to the
Animikie. Cavrltonian is suggested as a local name for the
formation.

In view of these conflicting opinions, the writer was in-
structed to make a detailed examination of the field relations
of the anorthosytes and the associated rocks. While engaged
in this work all of the localities, except Carlton peak, men-
tioned in Bulletin No. 8, as well as all the outcrops existing
farther inland, were examined. The following notes bear
chiefly upon the areas of the anorthosyte existing farther in-
land, and not described before. These observations confirm
the views of N. H. Winchell, Irving, and others, in that they
considered the anorthosyte masses as detached blocks inclosed
in later trap rocks.

The geological relations of the inland anorthosyte areas are
much clearer than of those at the lake shore, and, as will be
found in the following pages, susceptible of only one interpre-
tation, and the former masses have the same surroundings as
those of the latter. Excluding the opinions of previous writers
and interpreting the common facts of a part of the formation
by the facts common to the whole. an explanation totally dif-
ferent from that of Dr. Lawson must be assigned to the anor-
thosyte.

In the S. W. 4 of sec. 10, T. 55-8, at the top of the northward
facing bluff, 600 feet above the lake, are large masses of anor-
thosyte embedded in the black gabbro of the region. The
black rock here forms a perpendicular wall one hundred feet
high. The anorthosyte occurs only at the top of the ridge; it
is surrounded and cut by the diabase. The contact between
the two rocks is somewhat irregular and the anorthosyte has
the appearance of large irregular masses, rather than that of
a water-worn boulder or hilltop. Many of the large blocks
have been separated from the enclosing rock and also broken
in to smaller blocks, mainly through the action of recent ice in
the cracks, and finally have fallen over the bluff. One block
fifteen feet in diameter has been lifted partly out of its bed of
diabase, leaving an irregular basin several feet deep, which
was nearly full of water at the time. On the south slope of the
same ridge in the S. E. 4 of sec. 10, are several large masses of
anorthosyte. These appeared as though they had been rolled
down from the top of the ridge.

Both of the above occurrences are on the western extension
of the range which has been mentioned in the following: ‘‘ Be-

176 TWENTY-SECOND ANNUAL REPORT

tween Beaver Bay and the Great Palisades are numerous feld-
spar masses, in the coast series, and inland from the shore a
very short distance is a range of low hills made up of feld-
spar, with traprock on the flanks.”* The Beaver river breaks
through this range and precipitous bluffs of black olivine gab-
bro along both sides of the stream plainly show that this is
the only rock forming the range at this place. Masses of an-
orthosyte of all sizes occur enclosed in the black rock. The
flows of felsyte cover the gabbro and the anorthosyte. In the
east $ of sec. 1, T. 55-8, on the summit and the south slope of
the ridge are several large masses of anorthosyte. Thesouth-
ern slope of the ridge is heavily wooded and the rock outcrops
are for the greater part concealed. In ascending the ridge
from the lake shore nearly to the top the occasional outcrops
are black gabbro or diabase. The anorthorsyte at the top is
cut and surrounded in numerous places by the black gabbro.

Toward the north, the ridge breaks off abruptly in precipices
twenty-five to fifty feet high. The rock is always the black
gabbro which continues in extensive outcrops north of here.
In the N. E. tof N. W.iof sec. 12, T. 55-8, large irregular
masses of anorthosyte are enclosed in the black gabbro, which
forms a perpendicular wall fifty to a hundred feet high run-
ning at right angles to the trend of the ridge. The black
rock was traced northwestward into the valley north of the
ridge. This plainly shows that the mass of the ridge is made
up of this rock, and that the anorthosyte here simply forms a
mass, capping the black gabbro. Going east on the ‘‘old
county road” the ridge just mentioned is crossed, and for several
miles the road runs along the base of a northward facing
precipice of black gabbro, which forms the northern side of
the ridge.

There are several breaks in the ridge where good cross
sections were obtained, viz., along the creeks in section 31, T.
56-7, sections 19 and 20, sections 17 and 16, and along the Bap-
tism river in sections 4,10 and 15. Along these sections are
continuous outcrops of black gabbro having in some places a
coarsely bedded appearance, but usually massive. Anortho-
syte masses occur frequently at the top and on the south slope
of the ridge. A number of these have fallen over the bluff
into the valley on the north. In theS. E. 4 of sec. 8, T. 56-7,
the anorthosyte masses are as large as fifty to one one hun-

*N. H. Winchell, 9th Ann. Rept., p. 34, 1880.

Coed

STATE GEOLOGIST. iW aA

dred feet thick and three to five hundred feet wide, in one case
covering the surface for an eighth of a mile. The black gab-
bro cuts these masses, and forms the base of the ridge.

In the N. E. + of S. E. 4 of sec. 27 and the N. W. tof S. W. +
of sec. 26, T. 56-8, is an oblong ridge, one fourth of a mile long
and one eighth of a mile wide at the the top and three hundred
feet above the surrounding country and six hundred feet above
lake Superior. The upper half of this elevation is composed
of anorthosyte resting upon a base of the black gabbro of the
region, dikes of which cut the anorthosyte, which here is found
to vary in mineral composition considerably more than in other
localities. Itisnota pure feldsparrock. A large part of the rock
contains numerous dark areas of the ferro-magnesian minerals.
The whole rock has the composition of the normal gabbro.
Specimens 188a to g represent the different phases of the rock.

One half a mile northwest of this locality, in the S. E. + of N.
EH. 4+ sec. 27, is Schaff’s hill. The greater part of this hill is
composed of dark diabase, which forms perpendicular walls on
all sides of the hilland makes the ascent to the top very diffi-
cult. On top of the hill and near the southwestern edge is a
mass of anorthoryte about five hundred feet square. This is
the same pure feldspar rock which occurs at Beaver Bay. This
outcrop, six hundred and twenty feet above and four miles
from lake Superior, is the most distant outcrop of this rock
from the lake. Other occurrences are in the N. E. ¢ ofS. EH.
4 sec. 26, and-the S. W. ¢ sec. 25, T. 56-8. At both of these
localities there is no doubt that they are enclosed masses. In
the latter place an irregular mass of anorthosyte seventy feet
in diameter has been broken off from the neighboring diabase
wall and lies near its original place in a tilted position.

After these occurrences of the anorthosyte were examined
the most important exposures at Beaver Bay on the lake shore
were again examined. All of these outcrops hold the same re-
lation to the diabases and gabbros of this region as that held
by the outcrops farther inland.

The occurrence at the cove below Split Rock point is of im-
portance, and there exists a difference of opinion concern-
ing it. All geologists agree that the smaller masses of anor-
thosyte are fragments included in the diabase. Various views
have been expressed concerning the large masses.* The lim-
ited extent and the relations of the anorthosyte are apparently
the same as observed elsewhere. In this locality the relations

*Bulletin No. 8, pp. 11-14.

178 TWENTY-SECOND ANNUAL REPORT

of the different rocks are somewhat indistinct. Viewed in the
light of the other occurrences of even greater extent, whose
geological relations are undoubted, it is safe to place the rocks
in this locality in the same position. The hypothetical section
of the rocks at Split Rock point, given in Bulletin number 8,
p. 12, in no way represents the relations of the anorthosyte to
the later rock, as understood by the writer.

The mineralogical composition is not as constant as is
stated in Bulletin No. 8. Attention has been called to this
fact by Prof. Winchell* in the following note: ‘‘ That some of
the masses were not of pure feldspar rock, but contained in the
usual proportions, the minerals augite and magnetite. * * *
Thin sections have revealed in the feldspar boulders, however
pure they may appear to the eye, small quantities of augite,
and from these minute quantities there are all gradations to
typically constituted gabbro.” These statements the writer,
after his extended observations, is able to confirm.

In addition to the above, attention may be called to the fact
that in the majority of cases the original ferro-magnesian
mineral has been altered to chlorite, often forming a pseudo-
amygdaloidal structure. 188f in thin section shows this char-
acter. The most typical outcrop of the anorthosyte is the
ridge in the S. E. + sec. 27, T. 56-8. In this large mass all
variations and gradations described from different isolated lo-
calities are readily seen. Specimens 188a to g from this ridge
represent all the varieties, and may be taken as a typtical set
of the anorthosyte of the lake Superior coast.

Sufficient evidence has been presented to show that the
anorthosyte occurs only as included masses in the diabases and
that it does not represent a pre-Keweenawan terrane existing
in situ beneath the diabase. Conclusions based upon this as-
sumption have therefore no value. ;

The petrographical characters are the same as those of the
central part of the gabbro formation. Considering the gabbro
as the intrusive and the diabases as the effusive portions of the
same magma, it is easily seen that while the upper portion of
the magma was solidified as the gabbro, in the interior of the
mass large masses or aggregations of feldspar were separated.
These solid masses fioating around in the liquid magma were
ejected with it and, being considerably lighter than the sur-
rounding molten mass, floated near the surface and are there-
fore at present only found near the top of the first outburst of

*Bull. VIII, p. xviii.

STATE GEOLOGIST. 179

diabase. Later, when some of this diabase was eroded, the
feldspar knobs projected above the surrounding rocks and at
the time of the later lava flows were covered up by the felsytes ©
and other rocks of the red rock group. This explains the ori-
gin and present position as well as the domed and hummocky
characters of the anorthosy te.

VIII. SUMMARY.

In the preceding pages the writer has attempted to show
several points of interest to those who are working in the geol-
ogy of the pre-Cambrian rocks. A brief review of the more
important points advanced will not be out of place.

Snowbank lake area. The structure and some of the charac-
ters of the rocks north and west of the lake are given. The
quartz porphyry, so common in the Keewatin, here has an un-
usually extensive developement. An augite granite is de-
scribed, with an explanation of the local occurrence of augite
granites in Minnesota. Additional evidence is given showing
the derivation of the mica and hornblende schists from the
Keewatin.

Actinolite magnetite schists from the eastern Mesabi. Descrip-
tion of the schists and their geological associates is given,
showing their derivation from a rock containing an original .
iron carbonate. These schists were greatly affected by the
gabbro. Therecognition of the true character of these schists
will establish an important analogical link between the Mesabi
and the Penokee series. It is also shown that the so-called
Pewabic quartzyte between Birch lake and Gunflint lake be-
longs to the middle member (iron-bearing) of the Animikie.

The gabbro. Several observations in the hitherto unexplored
regions are recorded. Attention is called to the varying min-
eralogical phases of the gabbro showing that it is to be consid-
ered as an intrusive rather than an effusive.

The red rock. Augite syenite, quartz porphyry, felsyte, etc.,
are described from the vicinity of Greenwood lake. These
rocks were traced into similar rocks on the shore of lake
Superior. It is shown that nearly all of the red rock forms one
prominent group. The Keweenawan rocks north of lake Super-
ior are divided into the gabbro, diabase, red rock and the later
dike groups. |

The diabases. Under this group are included the fine grained
gabbros and diabases immediately south of the main body of
the red rock group. It is also suggested that the subdivisions

180 TWENTY-SECOND ANNUAL REPORT

of the Keweenawan of Minnesota into the minor groups‘ of
Irving is impossible. The diabases are considered as the
‘effusive equivalent of the gabbro.

The anorthosyte. Evidence is produced showing that the
anorthosyte occurs only as included masses in the diabases. In
mineralogical composition it is the same as the gabbro of which
it was originally a part. The anorthosyte occurs near the top
of the first outflow of the diabase group and afterwards it was
also covered by the felsyte and diabase of the red rock group.

The conclusions based upon the supposition of Lawson that |

the anorthosyte formed a pre-Keweenawan terrane are thus
rendered valueless.

XIII.

LIST OF ROCK SAMPLES COLLECTED IN 1893

By A. H. ELFTMAN.

The greater part of these specimens have been examined in
thin section. The term ‘‘anorthosyte” is used to designate the
pure feldspar rocks of the Keweenawan. These specimens are
marked with white shellac figures with the letter E after the
number.

1. Dioryte inclusion in granite. S. W.1N. W. }sec. 1, T.
62-12.

2. Schistose inclusion in granite. Same locality.
3. Contact of hornblende schist and granite. Same locality.
4. Porous condition of schists. Same locality.
5. Diabasedike. S. W. iS. E. 4 sec. 24, T. 62-12.
6. Granite near the preceding.
7. Lenticular hornblende mass in granite. N. EH. 4S. BE. }
ce. 25, T. 62-12.
8. Quartz dioryte inclusion in granite. 4 specimens. N. W.
+N. E. + sec. 7, T. 62-11.
9. Granite. Same locality.
10A. Gneiss. Inclusions in granite. S. E.4N. W. isec. 7,
T. 62-11.
10B. Contact. Same locality.
11. Quartz dioryte inclusion in granite. S. HE. 4S. E.4 sec.
12, T. 62-12.
12. Diabase dike. Same locality.
13. Dioryte. Same locality.
14. Fine grained granite. S. HE. +N. E. }sec. 13, T. 62-12.
15. Coarse granite. Same locality.
16. Schistose dioryte. N. H. iN. E.4sec. 18, T. 62-12.
17. Hornblende inclusion in granite. From the point on
White lron lake in S. W. 4S. W. 4 sec. 12, T. 62-12.
°18. Hornblende schist. Same locality.
19. Dioryte. Same locality.

182

20.
21.
22.
23.
24.
25.
26.

28.
Zo,
30.

dl.
d2.
33.

df.
30,
36.

9°

ol.

38.
39.
40.
41.
42.
43.
44.
45.

46.
47.
48.
49.

49.
00,
51.

D8.
o4.

ay)

56.

TWENTY-SECOND ANNUAL REPORT

Quartz. 200 paces north of S. E. corner sec. 11, T. 62-12.

Granite. Same locality.

Magnetite vein cutting granite. Same locality.

Magnetite. Same locality.

Light red granite. N. E.4N. E. 4sec. 14, T. 62-12.

Dark red granite, Same locality.

Weathered granite. Same locality.

Mica schist: S. W.4N. E. 4 sec. 35 T. 63-11.

Schist. N.E.4N. W. 4sec. 2, T. 62-11.

Mica schist. Same locality.

Concretionary greenstone. N. H. ¢ N. E. 4 seciatge
63-9.

Diabase. Same locality. :

Schistose diabase. Same locality.

Diabase dikes. a. Coarse, b. fine grained. N. W. iN.
E. + sec. 17, T. 63-9. .

Tale schist. N. W. iN. E. i sec. 17, T. 63-9.

Jasper. S. W.4S8S. W.4sec. 1. T. 63-10.

Schistose diabase. One foot from contact with jasper.
Same locality.

Diabase. Twenty feet from contact. Same locality.

Diabase. Forty feet from contact. Same locality.

Dioryte. S. W.4N. W.4sec. 31, T. 64-9.

Hornblende porphyry. S. W. 458. W. 4sec. 1, T. 63-10.

Schistose greenstone. Same locality.

Concretions in greenstone. Same locality.

Hornblende porphyry. N. E.;S. E.4 sec.31, T. 63-9.

Conglomerate. N. W. 4S. E. 4 sec. 31, T. 63-9.

Quartzless porphyry pebble in conglomerate. Same
locality.

Laminated diabase. N. E.48S. W. 14sec. 31, T. 64-9.

Matrix of conglomerate. Same locality.

Dioryte. Same locality.

AtoE. Quartz porphyry. S. W.iS.E.4 sec. 31, T.
64-9...

FandG. Weathered surface of the preceding.

Diabase. Same locality.

Contact of diabase and quartz porphyry. Same locality.

Jasper. N.W.4S. W. 4 sec. 32, T. 64-9.

Hornblende porphyry. Same locality.

Coarse dioryte. N. E. 2S. W. isec. 32, T. 64-9.

Quartzless porphyry. S. E. + N. W. 4 sec. 26, T. 64-9.

Granite cutting porphyry. Same locality.

STATE GEOLOGIST. 183

57. Quartzless porphyry. Same locality.

58. Contact of schist and porphyry.

59. Quartzless porphyry. N. H.4N. W. 4sec. 26, T. 64-9.
60. Quartz porphyry. N.E.4S. W. }sec. 23, T. 64-9.

61. Quartzless porphyry. 5. E.48S. W. 4sec. 23, T. 64-9.
62. Hornblende schist. N. W.+S. E. 4 sec. 23, T. 64-9.
63. Argillyte. S. W.48S. E.4sec. 34, T. 64-9.

64. Gabbro: N. HE. 4S. W. sec. 4, T. 63-8.

65. Gabbro. (Iron ore near bottom of the beds). Same locality.
66. Gabbro. (Iron ore near the top). Same locality.

67. Eine grained gabbro in the ore bed. Same locality.
68. Keewatin schist inclosed in gabbro. Same locality.
69. Coarse weathered gabbro. Same locality.

70. Coarse gabbro. S. H.4S. W.1 sec. 4, T. 63-8.

71. Gabbro, largely plagioclase. Same locality.

72A. Olivine gabbro. S. W. 4S. W. +sec. 4, T. 63-8.
72B. Bedded olivine gabbro. Same locality.

73. Contact of olivine and coarse gabbro. Same locality.
74. Diabase. N. W.45S. W. 4 sec. 34, T. 64-8.

75. TIronore. N. EH. 4S. W.isec. 4, T. 63-8.

76. Anorthosyte. N. W.1N. EH. 4sec. 24, T. 63-9.

(7. FEeldspar from No. 76. Same locality.

78. Specimens showing weathering of the gabbro.

79. Diabasic anorthosyte. S. HE. +N. W. 4sec. 24, T. 63-9.
80. Shows large plagioclase crystal in No. 79.

81. Olivine gabbro. N. W. iS. W. i sec. 20, T. 63-8.

82. Coarse olivine gabbro. Same locality.

83. Transition of Nos. 81 and 82.

84. Olivine gabbro. Same locality.

85. Olivine gabbro. N. W. 48S. E.4 sec. 1, T. 62-9.

86. Intermediate between Nos. 85 and 87.

87. Olivine gabbro. N. E.:iS. W.4see, 1, T. 62-9.

88. Granite dike. S. EH. 48S. W. 4sec. 1, T. 62-9.

89. Anorthosyte. S. H. 48S. W. 41sec. 1, T. 62-9.

90. Plagioclase crystals. N. W.i+of N. W.4 sec. 13, T. 63-8.
91. Plagioclase and diallage. Same locality.

92. Diallage. Same locality.

98. Olivine gabbro. S. E. corner sec. 1, T. 62-9.

94. Anorthosyte. N. W.3N. E. i} sec. 12, T. 62-9.

95. Olivine gabbro. N. W. 4S. W. 4 sec. 8, T. 62-8.

96. Diallage. S. W.4N. E.4 sec. 2, T. 62-9.

97. Gabbro. N. W.4N. E. 14sec. 29, T. 63-9.

98. Fine grained gabbro. Same locality.

184

30
100.
101.
102.

108.
104.
105.
106.
107.

108.

109.

110.

aA 1,
112.

113.

114.
115.
116.
117.

118.

19;
120.
121.

122.
123.
124.
125A.
125B.
126.

127.

128.
129.
130.
131A.

131B.
132.
133.

TWENTY-SECOND ANNUAL REPORT

Gabbro. Same locality.
Foliated olivine gabbro. Same locality.
Olivine gabbro. Same locality.
Contact between Nos. 97 and 100. N. E.3N. W. 4 sec.
29, T. 63-9.
Contact showing biotite in gabbro. Some locality.
Olivine gabbro. N. W.4N. E. 4 sec. 21, T. 61-9.
Olivine gabbro. S. W.3N. W. 14sec. 31, T. 62-9.
Olivine gabbro. N. W.4S. E.4sec. 7, T. 61-9.
Foliated diabasic gabbro. S. W.1sec. 12, T. 61-10.
Fine grained olivine gabbro. Same locality.
Olivine gabbro. Same locality.
Foliated olivine gabbro. S. E. 4S. E. 4 sec. 27, T. 62-10.
Bedded olivine gabbro. Same locality.
Olivine gabbro. N. W.iS. E.4sec. 27, T. 62-10.
Anorthosyte. Same locality.
Anorthosyte. 100 paces north of No. 113.
Anorthosyte. S. W.4N. E.4sec. 27, T. 62-10.
Plagioclase crystal in No. 115.
Olivine gabbro. S. W. iS. W. 4 sec. 15, T. 62-10.
Granite. N. H.4N. E. isec. 25, T. 62-8.
Contact between gabbro and granite. Same locality.
Olivine gabbro. S. E. 4 N. E. 4 sec. 20, T. 62-10.
Coarse gabbro. 100 feet north of magnetite ore. N. W.
i§. E. sec. 30, T. 62-10.
Infiltrated quartz. S. E.4S. E.4sec. 30, T. 62-10.
Pyroxenyte. Same locality.
Quartz and gabbro. Same locality.
Olivine. Same locality.
Hornblende. Same locality.
Olivine gabbro. Muskrat lake. S. W.1S. E. 4sec. 30,
T. 62-10.
Olivine gabbro. Muskrat lake. S. E.4S. H. }sec. 30,
T. 62-10.
Gabbro. S. H.iS. W. i sec. 29, T. 62-10.
Matrix of conglomerate. N. E. +S. W. i sec. 26, T. 64-9.
Dioryte. S. E. 48S. W. 4 sec. 18, T. 64-9.
Concretionary schistose diabase dike. N. E. corner
sec. 28, T. 62-11.
Contact of granite and dike.
Granite with part of dike adhering.
Granite. S. W. corner sec. 28, T. 62-11.

134.

135.
136.
137.
138.
139.
140.
141.
142.
143.
144.
145.
146.
147.

148A.
148B.

149A.
149B.

150.

151A.

151B.
151C.

152.

153A.
153B.

154.
155.
156.
157.
158.
159.

160.
bor:
162.
163.
164.
165.
166.

STATE GEOLOGIST. 185

Coarse foliated hornblende granite. N. W. 4 N. W. { sec.
33, T. 62-11.

Gabbro boulder. N. 4 post sec. 28, T. 62-11.

Granite. E. + post sec. 32, T. 62-11.

Orthoclase crystals. Same locality.

Orthoclase crystals. N. E.4N. E. }sec. 28, T. 62-11.

Coarse gabbro. S. W.458S. W. }sec. 19, T. 61-11.

Diabase. Same locality.

Slate boulder. Sec. 24, T. 61-12.

Pyroxenyte. Same locality.

Gabbro. Same locality.

Gabbro with chalcopyrite. Same locality.

Magnetite, sec. 24, T. 61-12.

Olivine gabbro. N. W. }sec. 31, T. 61-10.

Anorthosyte. N.H.4S. W. 4sec. 36, T. 61-11.
Anorthosyte. S. W.4N. W. isec. 31, T. 61-10.
Olivine and plagioclase segregations in gabbro. Same

locality. .
Anorthosyte. Harris lake. N. W.1 sec. 26, T, 61-11.
Olivine gabbro. Harris lake. N. HK. 4 sec. 27, T. 61-11.
Biotite gabbro. N. W.4sec. 29, T. 61-11.
Contact between feldspar and olivine segregations. N.
H. iN. E. + sec. 6, T. 60-11.
Laminated weathered surface of No. 151A.
Diallage. Same locality.
Anorthosyte. N. W.4S. W. 4 sec. 8, T. 60-11.
Olivine gabbro. N. 4+ post sec. 2, T. 60-10.
Olivine gabbro. N. W. i sec. 35, T. 61 10.

Anorthosyte. S. W.iN. W. 4 sec. 35, T. 61-10.

Olivine gabbro. N. ; post sec. 3, 'T’. 60-10.

Olivine gabbro. N. E.4N. E. 4 sec. 4, T. 60-10.

Gabbro. S. W. 4 see. 4, T. 59-10.

Diallage. Harris lake. Sec. 26, T. 61-11.

Olivine gabbro. 100 paces west of N. E. corner sec. 1,

T. 59-10.

Olivine gabbro. S. E. iN. E.4 sec. 1, T, 59-10.

Gabbro. 500 paces 8S. of E. + post sec. 1, T. 59-10.

Granite. Bootlake. S. W.iN. E. }sec. 21, T. 64-8.

Spotted talc schist. N. W. 45S. E. } sec. 15, T. 64-8.

Spotted tale schist. N. E. 4S. W. 4 sec. 22, T. 64-9.

Tale schist. Same locality.

Spotted schist. Same locality.

186
167.

168.
169.
170.
171A.
171B.
172.
173A.
173B.
174.
175.
176.
1.
178.
179A.

179B.
180.

TWENTY-SECOND ANNUAL REPORT

Schist with large orthoclase crystals. Same locality.
Preceding 4 specimens are transitions from 164 to 167.
Quartzless porphyry. S. W. 4 N. W. 4sec. 21, T. 64-8.
Ferruginous tale schist. S.E 48. W. 4 sec. 20, T. 64-9.
Gabbro. N. } part sec. 4, T. 60-8. [ Lost. ]

Diabase. N. W. iN. W. 4 sec. 36, T. 60-8.

Diabase. S. W. 4 N..W. 4 sec. 36, T. 60-8.
Black felsyte porphyry. N. + postsec. 31, T. 53-7.

Red felsyte porphyry. Same locality.

Weathered surface of No. 173A.
Laminated felsyte. Same locality.
Olivine gabbro. S. E.4+S. E. 4 sec. 30, T. 59-10.
Hypersthene gabbro. S. E. 1sec. 32, T. 59-10.
Gabbro veins. S. E. 4+ sec. 19, T. 60-8.
Hypersthene gabbro. Greenwood lake. N. E. 4 sec. 9,

T. 58-10.

Reddish gabbro. N. E.4sec. 16, T. 58-10.

Olivine gabbro. Same locality.
Augite syenite dike. Same locality.

181A to HE. Felsyte. N. E.4S. E. 4 sec. 33, T. 58-10.

182.
183.
184.
185.
186.

187.

188.

189.
190.

19%:
192.
193.
194.
195.

196.
197.

Felsyte porphyry. N. W.4 sec. 3, T. 57-10.

Diabase. N. W. }sec. 3, T. 57-10.

Felsyte porphyry. S. E.4S. E. 4sec. 1, T. 57-11.

Augite syenite. N. E. 48S. E. 14sec. 25, T. 58-10.

Augite syenite. 50 paces south of N. W. corner sec. 30,
T. 58-10.

Gabbro. ‘‘Grandmother” hill. S. W. 4S. E. 4sec. 8,
fas eb ESS

Anorthosyte. N. E.4S. E.14 sec. 27, T. 56-8. a Light
colored. 0 Shows fracture. c Dark colored, d
Chlorite segregations. e Weathering. jf Fine
grained. Chlorite evenly distributed.

Gabbro cutting No. 188.

Anorthosyte, shows weathering and chlorite. Schafti’s
hill. S. W.4N. E. 4 sec. 27, T. 56.8.

Gabbro. Schaff’s hill.

Diabase at top of hill. S. W. 34S. E.4sec. 22, T. 56-8.

Diabase north base of hill.

Diabase. In river bed. N. W.4S. E.4 sec. 22, T. 56-8.

Amygdaloidal diabase, laumontite, chlorite, calcite and
quartz. Same locality.

Diabase porphyryte. S. W. 4S. E. 14sec. 22, T. 56-8.

Diabase. Same locality.

198A.
198B.

199.
200.
201.
202.
203.
204.

205.
206.
207.
208.
209.
210.
211.
212.

213A.

213B.

214.
215.
216.
217.
218.
219.
220.

221.
222.
223.
224,
225.
226.
227.
228.
229.
230.
231.
232.
233.
234.

STATE GEOLOGIST. 187

Red mottled gabbro. S. E.4S. W.4sec. 34, T. 57-7.
Diabase. S. E.45S. E. } sec. 34, T. 57-7

Gabbro. S. E.iS. W. 4sec. 27, T. 56-8.

Gabbro. S. E.45S. W. i sec. 11, T. 56-8.

Gabbro. N. H.iN.E. + sec. 18, T. 56 8.

Diabase. N. W. 45S. W. 4 sec. 7, T. 56-7

Diabase ee irnee. Same locality.

Gabbro containing plagioclase crystal 1 inch in diameter.
N. E. 4 sec. 6, T. 56 i

Gabbro. N. W.iN.E. 4sec. 6, T. 57-7.

Gabbro. S. E. 4 sec. 19, dhs Ere

Gabbro. N. W. iN. W. isec. 25, T. 56-8

Diabase. N. W. iS. W. isec. 25, T. 56-8.
Anorthosyte. N. E.4S. HE. 4 sec. 26, T. 56-8.

Red gabbro. N. HE. 45S. W. 4 sec. 25, T. 56-8.
Diabase. Bear lee N. W. i N. W. t+’sec. 3. T. 55-8

Diabase. N. E.iN. W. 4sec. 3, T. 55-8.
Amyegdaloidal idugthase porphyryte. On town road,
mile south of N. E. corner sec. 8, T. 55-8.
Same, one half mile south of the preceding.
Diabase. S. E.iN. W. isec. 31, T. 56-8.
Gabbro. 50 vaces south of N. W. corner sec. 15, T. 56-9.
Diabase porphyryte. N. H.4N. EH. 4 sec. 9, T. 55-8.
Diabase. S. W. 14S. E. 4 sec. 9, T. 55-8.
Diabase. S. E. 15S. EH. 4 sec. 9, T. 55-8.
Anorthosyte. S. E.48S. W. 14sec. 10, T. 55-8.
Olivine gabbro. Second falls of Beaver river. N.W.+
S. W. 4 sec. 12, T. 55-8.
Fine grained diabase. N. W.48S. W. 4
Amygdaloidal diabase. S.E.48. E.4
Gabbro. N. W.4N. W.4 Bee: 1, T. 55-8.

BIH

Anorthosyte. S. W.+S. "E, 4 ec. 1, 'T. 55-8
Augite syenite. S. W. f sec. 5, T. 57-7.
Diabase. S. W. 4N. ce + sec. 22, T. 57-7
Olivine gabbro. W.4 Post sec. 35, T. 55-11
Diabase. S. W. iN. E eae 33, T. 55-10.

Diabase. S. E.iS. W. 4+sec. 11, T. 55-10.

Anorthosyte boulder. Sime locality.

Diabase. N. W.iN. EH. isec. 15, T. 55-10.

Diabase. N. W. +N. W. }sec, 23, T. 55-10.

Diabase. S. E. 4S. E. 4+ sec. 26, T. 53-11.

Ophitic gabbro. 100 paces north of S. EK. corner sec. 27,
T. 53-11.

188

235.
236.

237.
238.
239.
240.
241.
242.
243.
244.
245.

246.
247.

248.

249.

Or
2

CTU SS St COU car

bo ps DO PDO MH bO PO PW WO
SI OU oo Po

or or Ol
OO
>

TWENTY-SECOND ANNUAL REPORT

Ophitic olivine gabbro. Same locality.

Contact between 235 and anorthosyte inclusion. Same
locality. 2

Fine grained red gabbro. N. E. 4 N. E.4sec. 34, T. 53-11.

Diabase. N. W. 4S. W. 4 sec. 12, T. 53-11.
Diabase. N. HE. 4 N. E. 3 sec. 17, T. 53-11.
Diabase. S. W. iN. W. isec. 8, T. 53-11.

Diabase with feldspar crystals. Same locality.
Compact felsyte. Railroad cut. N. EH. ¢sec. 21, T. 52-11.
Amygdaloidal diabase. Lake shore, sec. 21, T. 52-11.
Diabase. S. W.4N. W.4 sec. 8, T. 53-11,
Amygdaloidal diabase containing laumontite, calcite, etc.
Stewart river, S. W. 4 .N, E. 4sec. 29, T. 53-10.
Amygdaloidal diabase. From ‘‘copper mine.” S. EH. 4
N. HE. 4 sec. 29, T. 53-11.
Fine grained phase of 246.
4 specimens represent the rock below the amygdaloidal
diabase, and form bed of the Stewartriver. N. E. +
N. W. 4 sec. 29, T. 53-10.
Diabase. Upper falls (‘the slide”) of Stewart river.
N. W. 45S. W. 4 sec. 20, T. 53-10.
Gabbro. S. W.iS. W. + see. 15, T. 53-10.
Diabase. Mouth of Stewart river.
Gabbro. N. W.1S. W. 4sec. 4, T. 53-10.
Diabase. Same locality.
Contact between Nos. 252 and 253.
Gabbro. N. W. sec. 6, T. 54-9.
Amygdaloidal diabase. Point below Split Rock river.
Diabase. First falls of Gooseberry river.
Diabase. Flood bay. S. E.4N. W. 4 sec. 32, T. 53-10. —
Laminated diabase. Same locality.
Diabase. Rock cut two miles north of Highland. D. &
I. R. railroad.
Diabase. N. W. corner sec. 12, T. 52-11.
Fine red mottled diabase. Lighthouse point at Two
Harbors. ;
Diabase. Rock cut one mile north of Two Harbors.
A different phase of No. 262. 7 wean 8.
Diabase. One mile south of Cloquet. . \
Red rock boulder. Same iocality. :
Diabase. On old county road north of Great Palisades.
Quartzless porphyry. S. E. 1S. E. 4 sec. 23, T. 64-9.
Granite. Same locality. ©

269.
270.
271.
272.
273.
274.

275.
276.
277.
278.
279.

280.
281.
282.
283.
284.
285.
286.
287.
288.

STATE GEOLOGIST. 189

Schist. S. HE. +N. W ¢isec. 24, T. 64-9.

Quartzless porphyry. N. E. 4S. E.14 sec. 19, T. 64-8.

Augite granite. N. W.3S. W.isec. 20, T. 64-8.

Quartzless porphyry. S. W.4N. W. 14sec 20, T. 64-8.

Granite. S. W.1N. W. + sec. 20, T. 64-8.

Siliceous schist. Boot lake. N.W.1S.E.4 sec. 21, T.
64-8.

Granite. S. W.4N. W. 1sec. 20, T. 64-8.

Matrix of conglomerate. N. E. $S. E. 4 sec. 22, T. 64-9.

Argillitic schist. Sarne locality.

Dioryte. N. E.458. W. }sec. 28, T. 64-9.

Quartzless porphyry. Flask lake. S. E. 1S. E.isec.
28, T. 64-9.

Dioryte. Same locality.

Hornblende porphyry. 8S. W.iN. W. 4sec. 31, T. 64-9.

Hornblende schist. Jasper lake, sec. 1, T. 63-10.

Hematite. S. W.4S. E. 4 sec, 1, T. 63-10.

Hornblende porphyry, Same locality.

Dioryte. N. W.iS. W. isec. 26, T. 64-9.

Argillitic schist. N. HE. 18S. W.isec. 26, T. 64-9.

Spotted tale schist. N. W. 4S. EH. }sec. 15, T. 64-8.

Diabase. Bed of Baptism river at the crossing of the
old county road. S. H. 4sec. 4, T. 56-7.

ER eS ME NS Ee ees MOS Seas Meee sor as. ae OR Ee eng eye S65)
* rt ie Bear, “Rho . Card ie aS
- YR ots +8 cu 3. ee
Nd - ‘ £ % ‘ = oe
190 TWENTY-SECOND ANNUAL REPORT eae

Sa
aad OBTAINED. roe
eria co)
No a) a NAME, ee
When. Whence. 53
; An
7947 jAug., 1891)A. E. Foote.....|Diablo canyon meteoriciron................. if
7948 eS 3 23--iSilicedus. iron. 32 «ce: secs os ssa. 18 eee BY
7919 |Feb.. 1892/H. A. Wee Fayette county, Texas, meteorite Pe 1 slab
ca Sept., 1892)Donation...... pea from the rst iron furnace i in America e
; $e <P fecee | LOM: traty wee mE fi Be
7952 |Sept., 1893|/Dr.A. si hives h Carlton meteorite, slab, etched........... ad Dep
7953 e ES .|Bella Roca meteorite, slab, etched......... 1
795 Ey ¥ ..|Crab Orchard meteorite, slab.........+. +++ me
7955 ss - ..|Mercedetas meteorite. slab. etched..... ... uy
7956 a “ ..|Duncan meteorite, slab, etched.. ig 1
7957 |Feb., 1891)Presented ......|Magnetiticiron ore from crystalline schists wee
7958 ae x --..../|Granite 1
PO MAN, Ccctnacs cvbiwe| Cacuicvcete caacce op (Stratiied. yoleanic dubt (with casts of
grasses) .. DAs
JOGO Viet icnck aheOeel ks ta ceeds coseeec'| Rapple bedded volcanic dust (with pellets) 1
7961 |July 3,1892|Geol. Survey.:.|Beach stone, .:...... .i.iceeees, ose dcecee sabe ae
tel Eee ee A; BAM | Age h is =, see ee ae TALES ah Sie ot es oe eyes 2.
TO6S En Bek 2 aes : +! [Iron-ore.2) sea. J SA eee eae 1
1h a Petar teceeaten elec YC... o. cdc oe aoe Ly
7966 veces | Glacialiclay. .....525 saa. esgecs ce obese bee sone a
7967 Sep.20, 1889] Donated........ Sperrylite.:: 2.5 3... 50002. 0c nl ee ee en ee

7968 |Aug.7, 1892!/Geol. Survey. ..|Quartzyte, light gray...............sesse-0s 11

7969 |J’ne 20,1893 ¢ .--| Diabase, black. 2:5-2.1si--2--5:Senanees pte 5 ae
7970 “s & iv. sé sé ry a9 “

7971 |Oct. 17,1893 BS ...|Granite. gray, coarse ........ ssetanss teat eee 3 “ ;

7972 7 eS Fier oa rh “(with inclusions of
black hornblende schist) ............-+-.-- 9
7973 |Sep. 14,1893 J .../Schist, sericitic, weathered. ferruginous .. ta"
7974 |J’ne 19,1893 “s ...|Magnesian eau. eae) pyrititerdus a
a boulder.....,.22c0.--si0s do thes) alk eee i)
7975 |Aug.3, 1293 + .. |Pebbles, red, is igneous rocks ftom a E.
Miriniesota: «ib ona. aseote te «seeds sug ee sly Sn
Ps
. Ab
7976 2 “3 ...|Lignite, fragments in modified drift ....... 1
7977 + |Oct. 17,1893 i ...|Paconyte (20th Ann. Rep., p. 124), a fissile,|
slaty variety—from morainic drift...... Cy et
7978 1892 Ae ...|Diabase, coarse, magnetic. ...... .e0205 «oe A
“3
7979 f ¥ SIGADDIO; COATECLat sec ot oes ee oe pcos eeaee Ly
7980 c % PPahase ....9ckeepeee bees = 2 Wogoasies 248 aan 27%
7981 < dd * WIGPANILE, TEACISne oases» Lemp stape soe eee aioe Ne
aes
5982 J aS F J: ae Cet, - ord hka oie ae otktete mae 2 ee
7983 4 4 ™ |\Various rockS.:acse- ++. se oeypene <eeee 6 er
7934 1893 2 plhiBlate, black. ose acs es tee, mabiosie ash cneeeeee oo ;

STATE GEOLOGIST. 191

MINERALOGY AND LITHOLOGY.
MUSEUM SINCE THE LAST REPORT.

LOCALITY. Formation. COLLECTOR AND REMARKS,

Diablo canyon, Ariz PRAT eM wis Sverre oe Sandee 4 A.E. Foote. Weight 12% 0
RE ect pai oe sete c aster yale wae Found in connection with 7047, 734 OZ,
Fayette county, Tex A large polished slab, 22x11 in.
Lynn, Mass See eps nia tetiaiee: |\9 d:eidlefeiciareic/e sierra N. A. Winchell. From the old cinder piles.
oe Seat Roem Scolds cs he ad.cce BY Sechaba: 249 gr.
Durango, Mex.. Behtdeseiecl| dutissleleacea cele +: 210 gr
Cumberland Co, ‘Tenn. 388 cre0 dol to dC RR Gae eee 4 55 gr.
Beth felaicrafas |oatehaatingaterssias Gs 422 gr.
TRS aA a uf 118 gr.
N. of Long L,,St. Louis Co. »Minn Vermilion... Hillberg and Brandine.
McPherson Co., Kan.. Hotta rant mee eaeeies J. A. Udden.
Morrison’s bay,PigeonPt.,Minn|... ............|N. H. Winchell.
WEG TENT) \\ WC a re ees »..{Galena........|Chas. Schuchert.
1% m _ N. of Iron Ridge, Wis. fake. Clinton)....... ee ES
esha, Wis. isco Bam Fao ee Ie *
Sudbury, DE ae ee aR ee Present by F. L. Sperry.
N.W. side of Dam lake, Ait- {Kimberly).
kin Co.. near middle of W.% }+'Pewabic...... Warren Upham. (About 34 m. south of
SW if of see 8116 B95,Ait: | | [the foregoing).
| Kin Co. ashen outcrop... a ee 02 cu (About 3m. 8. W. from
Same loealiry, eastern outcrop. ACS cp OD Ae ICE 6 “ These outcrops are about

20 rods apart, the 2d and smaller being
N. E. from the first.
Hinsdale, D. & I.R railroad.

near center of S. % of sec. 8, Warran Upham. (Forming the Giant’s
T. 59, R. 14 W.; abandoned or “Mesabi’”’ range; quarried here for
PERN VE as ole tt alte ale eicya waive Aieia,o | [a/niaic«,2)cia seis wicieves the auditorium, Chicago.)

Same quarry with preceding...]................| Warren Upham. (Boulders of similar

granite, with such inclusions. sre found
rarely in southwestern Minnesota; for
examples in Big Stone and Otter Tail
counties, see vol. i, p. 625; and vol. ii,

Near S. E. cor. of sec. 20, T. 46, p. 551).
eo RO arltOn COUNLY?.. ..dcek |\s. sconce dodenc cs Warren Upham. (Close, W. of Kettle
river,on road from Moose Lake station
Hickory P.O., sec. 26, ss 46, R. to Beaver, Aitkin county.)
27, Aitkin county.. NGS anitt-2 5.6. Warren Upham. (Limestone boulders

are very rare in this country.)

Shore of Sandy lake, Aitkin)Mod. drift|Warren Upham. (Forming the greater
county, along road % m.south| (Kame pla-| part of the gravel.)

MMOLE Set eine ce sciecloeres dys ace naes| LOB Gravel)
Presented by Archibald Johnson, Super-

Excavation for Sandy lake intendent of Construction. (Plentiful
dam, Aitkin county........... Mod. drift....| in a bed of sand and gravel below the

level of the river.)

Mesaba station, D.& I. R. rail-|Gl. drift ..... Warren Upham. (Abundant in Knolly
road, near 8. E. cor. sec. 20, morainie drift here, and especially in
PEON ES LL feiss iadicteireiceiccas cs’ tee belt crossed by railroad 34-144 ms. §. E,

of Mesaba.)

Cormorant island (3 m. N. E. of}................ J.E. Todd. No.1.

Rocky point) Lake of the
WED UE aa

Rocky point (near Gunderson’s)}..... Jehes sees bh VOOdwaINO: 2.
fishery) | cepa of pe Meo).

Same locality... efi Bice derecho uy ee Odds .NOgo:

eC ee eee hae hea a alocic-ceeesteeeelonen.. roddy JNo, 4:.(Sample of layer;
vertical, 1-2 ft. thick at junction of

lela and granite. )
em MAT Mains Giga Miepel’ cra etsleialhe bine civ eaactee skies J.E. Todd. No.5. (Forming S. W. por-

Cormorant island, Lake of the — of Rocky point at Gunderson’s.
Woods. Moen ieetclsstseccioceses| ke Mee LOG INOS O

Rapia Mipee tas cir mes els Soiree. J. E. Toda.

192

OBTAINED.

’

TWENTY-SECOND ANNUAL REPORT

MUSEUM ADDITIONS
SPECIMENS REGISTERED IN THE GENERAL

Number of
specimens.

7992

7993

July 22,1893 Geol. Sapa hoe 7

1893

1892
July15,1893
1893

‘

...|Limestone. .. one wcee
.|Greenstone with rounded ‘quartzes.. Abas

Diabase ...... sciss 2s)-jem obs Seo aS ee

-\Granite. biotitic.. wsdealee
-|Mica schist, with ‘pegmatite veins sone

--|Diabase.. ccbows Hea np attest pee
..|Syenite, hornblendic wi Seo = ale 06/0 oo oe pa
-|Mica schist with pegmatite vein..... utiieese

ee Granite and diabase in contact........ .....
-|Dioryte with feldspar vein.................-

=| MiGa SChish....|./cn sere SECT Pe
- (Granite, SYAY....csssuctoersesterstee soon) Pao
-|Gneiss, COAFSC. .\.. .stcs-useeasceotoccdestoseee
-(Diabase.. 5. i: sosectspecteme russe reee eee

-.|Greenstone from boulder..................--
-|Limescone from boulder........... ........-

-| Various bouldersi.....c. fa > bs 4-s0= see
oo =| DIOKY tele. oa. cskeee stasentne Bee vile Sects amen
-|Dioryse) COATSC...: <<. sees oe:cacsesiny cots eeeee
«| DIONVPCS :. so +a Seeee S bhestle St cone: Gao
*| PHOLYEO. 025505 culawlael esos be oe an deen een
>| DIOTY60)ss2.< svc <cto easece bet eee ne eee sosteeeee

-.-|\Granite from dike in mica schist...........
-|Graphic granite... ..........ss0. sae oases
..2¢| GMCISS,; DIOGIUIC -2, —..cia hot Sora eet soiree ee
- |Granite; coarse, £rBy. ...<0. de oa selteee ne eeee
..|Granite with pegmatite vein......... 3 ieee
: Biotite granite,coarse.. pe saee (-Peee 8
ee fine.. v.59) Sie = piso stele

...|Granite, garnetiferous.. <iohp Coal diem aaa

“72 r coarse, greenish .......-2Jccsseaaens
-|Quartz vein rock........ acleweweswn epee ee
GLATIte: 20. os vice se cide een b boees ae eee
Miea schist, reddish.¢.~..©:i.-\.c<seeeeeles ales
.|Granite, gray, medium grained.. ..........
43 reddish, rather coarse.......... ..-

* COAPSO.acdacins co ea cin seeds paemen Meee
re Diotitio 7st eee Sates eee eee

si Mica schist..2 22 bc cobs sc odacekcos seer neensete
Granite: 2a SS eee sods eas
seni Mica SCHISH:2 3) no).cs aces cine poten Sete e becele Sees
5c | DOTY tO. «20: ooeeisaek terse < oem mebente es cnee eee

Diabase, magnetitic............cccce: sacs

.|Syenite, very fine grained, porphyritic...

Gray Wacke .. 200 foasces. sc veoh eee

mw ee

Cede taney oe aml Om pee) ae ecpeare tt

Hat COROMAHRTOODND tee CO et

Oty ar a ey cs

STATE GEOLOGIST. 193

MINERALOGY AND LITHOLOGY.
MUSEUM SINCE THE LAST REPORT.

LOCALITY. Formation. COLLECTOR AND REMARKS.
Peon Ori river. .paceeeeschecetscelssss «as----cas\d. Hp Lodd, (Locality. B.)
< ST. Sate aeite Stewles ..|\J. E. Todd. (Locality B.)
eS Set Teme een ete avsiaiete aial|l= cate saais lars oleai ocd J.E.Todd. (7or8 m. below junction of
Big Fork and Sturgeon rivers. )
44m. E.of mouth of Rapid river.|..............-. ee E odd.
Rocky point, Lake of the Woods; Sey Ree Ee “ [Elm Point.)
Long point. SO OS a ee eee &¢ = (Long Point is also called
Lake of the Woods, 8S. shore....|......-.....+.- < &s (Zipple’s house, near mouth
of Sand creek.)
ss ve és CO ee (on = Sa J.E. Todd. (Rock hummock 40 ft. high, 4

m. S. W. of Zipple’s, near the mouth of
Sand creek or Winter Road river.)
Big Fork river, % m. below

SE OMATIMEE te ac... cl: |escnee csc sscese-(d', Hr.) OGG.
Big Fork river, % m. below
e Sturgeon river................ 42 ASHP ACB EEA ee Dy
Big Fork river, % m. below ;
PIP COMELVOD Se. visces< cas. elec|ecteers lds» Seana Weis “
Big Fork river, 4-5 m. below
SEE OOTCET VOT ef ccc noc eee aclessaesmecdselc es | u** ** (Locality B.)
a SEE la i ee ARS eden * by
Mississippi river, 3-4 m. below
. PTE eae ee RD Sone gine * oe
N.E. of ition take E.Hubbard
LEWIN RS Sepa ene eee ‘ee Meatemates se cs =
Big Fork river, T. 61-26.. Ee -...... .|G. E. Culver. ‘‘First exposure on Big
Fork.” (Note B., p. 23.)
ae oa fs isos deelbawaeess teeta t1Geb.Culver. “Kirst exposure on? Big
Fork.” (Note B., p. 23.)
ee 8 BS AT eae 8 San bate oe ole aetee sidjole G.E. Culver. Probably from first expos-
ure on Big Fork. (Note B., P. 23.)
Ss * So 96) 2 or al Incouo uaoapooc G. E. Culver. Probably from first expos-
ure on Big Fork. (Note B., p. 23.)
ds sf Ce RARE pea het ee a eee Parse G. E. Culver. Probably from first expos-
ure on Big Fork. (Note B., p. 23.)
= rr Se RRS hal bore BeCoE A cieD G. E, Culver. Vein-like in form.
Big Fork river, % between Rice
PIE FTI VOUSs oe re oa. 8 osha nm cine ote" = == ue wo (Note B.. p. 28.)
Big Fork river, 4% m. below
POP COW TIVETA 2 nrerie- once ee ss|a00% vette at o/aies «- as - (Note B., p. 29.)
Big Fork river, % m. below
PIPES COM TLV GEe: 2.5 see's cern = jsdRor-proocace a es es “
Big Fork river, 1% m. below
PME COID TV ER) is soc dais sae d|'Paeh vee aa + wales 5 a BS *
Big Fork river, 10 m. below
Rig falls... Or OCT One | ates se Ss “¢
Between Stu: rgeon ‘and BigFork
rivers, 25 m. below Big TAVIS Niele s Giadases 5 G. E. Culver.
Big Fork river, 25 m. below Big
falls COS B RODS 52 BCL JC SEGRE ObG Cdl | SOP SOD DESC TEE SS o (Note B.,p. 40).
“se Cy EO OO IDE 5 sg Ce i
ep Se ha epee ed Balter ss (os sas)
S. line of sec. 33, 66-21............|...- ifs C. L. Chase. LN. of the granite.
W. line of see. 18, 66-21. se aS Mica schist is all along the
N. line of sec. 23, 66-21. se vd
W. line of sec. 18, 66-21. eS ss
-linemear N. edge)sec. 31,66- a apes ee :
Sec. 9, 66- 21 Pecisstue veces oo acs ve ss [granite.
ae eats oe a Ay opie <f Schist is on the N. of the
See’ s. 22, 23 and PEL Os ones Seas ot ee 9 eens a eet a ae Country is full of gran-

ite ridges. with intervening swamps;
the granite runs N. E.an

Sees 22,23 and, 24, 66-23. ..:..4...| 03 ONE: Chase. The schist lies to the N. of
S.E.% 3. E. % sec. 4, 56- Oe awe ee [the granite.
W. line ce 150 chs. N. of S.W.

CO tee Seg hick [ccs leas s Me ote ack Af + “StrikeS.70° W. Dip 8S. 70°”.
N. line sec. 11, 56-11........... Re} 2s ete coe ees es About 5 chs. W. of river;

about 25 chs. from E. corner.
C. L. Chase. On river.

“

S. W. 4S. W. % sec. 15, 56-11
Sec. 20, 64-21

i ad

194 TWENTY-SECOND ANNUAL REPORT
MUSEUM ADDITIONS
SPECIMENS REGISTERED IN THE GENERAL
Sa
OBTAINED. Pgh.
Serial NAME Se
No. r i)
When. Whence. =e
Zn
8031 1893 Donation.. 3| Ga DDIOs 2), ch fore. cechicshd skienie ns eee ata anne 1
3032 ey S jess s-|Diabase, fine grained... ......2-..-0 see 1
8033 dg ae .|Syenite, very “fine grained, porphyritic.. 2
MUSEUM ADDITIONS
SPECIMENS REGISTERED IN THE GENERAL
Sa
OBTAINED. ne
Serial NAME. a5
oO. °
When. Whence. =) 2
AD
[oe VA | Dia tie ea a Geol. Survey. ../ EndoOceras? «3 J. soc; wictelessiscseiee cee teen ?
ES aera . Hey PL in eee aero ree $3 eee diea's at Cee een “
8444 4g PE yl Sek ee Se ete a ptele Gielen are eet tee eae ae =
BAG N chek es See iat s ae Se gay lowe tack) Pilabta esos alee < Mace me
8446 |July, 1891 ne ...|Rhychonella neenah Whit..... ........... i 2
8450 |Sept., 1893 “s , .-|Aristerellanitidula llr. 2A... cee. cccce anaes 1
8451 = ss ...|Rhipidomella missouriensis... mete Are t 6
8452 a Z ...|Productella pyxidata Hall.................. 18
8453 #4 x ...,Chonetes geniculatus White..... e ll
8454 ef ss ..-|Cyrtina acutirostris Shumard.............. il
8455 ss + oe Chonopterium CMUSUWM 6 s.50 5) ee. nee eee rs
8456 i 2g ...|/Productus BD? ves wiee sae ceceine eens sneneceneces 5
8457 x ae ...|Phillipsia sp.?.. 2
8458 s ° _..|Cry ptoblastus melo O. & S.. cuptevioaceeae 2
8460 & uE .|Spirifera ae oor Shumard?...... 2
S461 ss . Phillipsia sp.?. enlsnes cAces tne 2 P
8462 = fs Platyceras sp.? ? 3
8463 es os Fish coprolite. . . 1
8464 + 2 Pleurotomaria sp.?.. oe She 4
8465 se Ue Piatyceras sp.? bad ded melawere Ree nice Ooch mee see 1
$466 zs * Zygospira? sp.? 14
8467 $y ss Cornulites carbonarius Gurley.. aeieldtocee ee 1
8468 _ ne ...|Palzeacis enormis M. and W...............-- 1
8469 “ c ...,Orthothetes lens.. ; 6
847 My : ...|Euompbhalus sp. ? (young of E. latus)... a 2
8471 “c a ...|Leptena rhomboidalis. .-.....:-...0+ «2.0... 3
8472 3: os ...|Zaphrentis ida A. Winchell.. BP dé 2
8473 a : .. jstrophalosia Scinbilla :2.. .\.5.-ssee eeeemene 1
8474 as ...,Orthis testudinaria Dalman SP Same 12
8475 se “s Mish teeth, gens 2. Spiess dec ovo eeteniee Bi ela! 5
8476 ‘ :..|Zaphrentis calceola W. hand W .2<hscceee 2
8477 es ae ...|\Spirifera marionensis Shumard............. 10
847 fe a5 .../Athyris hannibalensis Swallow............ 3
8479 & a .../Spirorbis kinderhookensis Gurley...... 1
8480 * pe ...|Terebratula burlingtonensis White... a 5
8481 Ee 2: : .0| ChOnEtES Ona tacks es ee ee eee re eee 6
8498 jAug., 1891 ...|Hindia sphenroidalis Duncan....... ...... 2
8499 : s .Raufella filosa Ulicla.. Sasi dco vedades ese 1
8500 ot oe ...|ISchadites iowensiS Owen..............--.--- 1
8505 ‘s $s .--|Rafinesquina alternata pees Mion SeHo6 36 1
8506 Es 2: » AOFthis subQguadratavHallsccs sce cea sear 3
8507 * . ... Strophomena filitexta Hall e330)... 1
8513 3: , .»-(Orthis meedsi Ww and\S. 00.050. 0.cxoece seed 2
8514 $s : ... Zygospisa uphami W. and S42 ducctvh tae 5
8515 ae be : Platystrophia biforata Schlot....... : 2
8516 ee & .. Orthis ? subeequata var. gibbosa Billings. 1
8517 Ke ge ’./Orthis testudinaria var. meeki..........-.- 1
8518 ss “ ...|Rhynchotrema inwquivalvis..............+. 5
8519 r es be cent aeeeee increbescens Hall . 2
8520 Es uP ., Orthis subequata var. perveta Conrad.. 1

STATE GEOLOGIST. 195

MINERALOGY AND LITHOLOGY.
MUSEUM SINCE THE LAST REPORT.

LOCALITY. Formation. COLLECTOR AND REMARKS,

(C. L. Chase. No. 8032 is in a wall 30 ft.
| high facing N. 50° E.; slopesS. 100
paces to the level of the ground. On

N. EB. YN. E. 4% sec. 4. 55-11......
oS Be _ -|{ the N.is No.8031,making a small ridge

weno

t Siaiie Dh Gn ta as | E. and W., separated from the last
by a ravine. No. 8033 isin a vein in
\_No. 8081.
PALEONTOLOGY.
MUSEUM SINCE THE LAST REPORT.
LOCALITY. Formation. COLLECTOR AND REMARKS.
11.2 ED se [ee eR Trenton Chas. Schuchert.
limestone

Minneapolis, Minn .............. 5 oy
OE ANI MA eaicey. Secheenl ra Chas. Schuchert.
Hader, Minn....... ..|Galena.. .....|Scofield and Schuchert.
Iron Ridge. Wis.. ....| Hudson River|Chas. Schuchert.

Ghataeld, Minn... 2.0.02. essect Trenton sh’l’s/Presented by E. O. Ulrich. Vol. III, p. 545.
Louisiana, WiGy5 se tie Se erate Lith.lim’st’ne R. R. Rowley. By exchange.
* Mbt eee eee eens sere e te rf 5 =
. Bante eens ees ec erates : 5 E ‘

if Be Sree era. 3 i =
Es Ait BEER aa ee L. Burl. ch ‘ :
rs * ad ce ce se oe
‘ oe = a - ‘
.: Mneteteneeeee ceeeee ms A :
se ay ee “sé ‘ ‘ *
+ Beene e te eeeeeeee ee 2 ; Es .:
oe 2 H Lith.lim’st’ne| ‘ Y rg
se ve “ we [74 . ao
i. BS nates eee eeeeees on at rr :, ci a
SS spaces sees eee ee eens re = y Z < *
of ee Ste Se cree <5 oe as ee os ‘. te
3 ew ttetreteeetteeereees 5 a is : ne ¥
‘ Ee RT fps anal BIE sono) bee &s 6s bs
Near Edgewood. Pike Co., Mo..|Clinton group| ‘“ hs ‘
deouisiana, MO... 222k... 2sece ? ~ 7
Ay ie SORE re on elena L.Burl. chert.) ‘ s ss Ee
ee x Breese eeiel< seen Looe mest nel. °° * rf +
ee “s iL Seek? 2 dg aia ee “oe oe . te
¥ Co eS OC eae L.Burl. chert.| “ a 4 ss
rs Baits torch ait andiers\s state eA Lith.lim’st’ne| ‘* ve e iH
MT Ae aioe oy tol. foie sin ci tiainalecteia'ns Niagara gr....|Scofield and Schuchert.
alaaaimepeie cla siie ie cteies cele eats Pere cloves feta ste| | ELIE Chewy eve I a,
Sete ictal elae'ate vais) atateis cer eisfa areicies Trenton sh’l’s
pte epee ett ae ein oe ie Lele wi Sais alee riem ¢ Galena shales
Seer otaln stor ate stalare evacts\ stole. Sie oj a cf ...|Lrenton sh’l’s
Stoke ASCE COAE CE PIER Ee nin an Hud. Riv. gr.,
Riese ialsinieeaier ei Viel chicies afte: shine, oo a ve a eisne rae Galena shale.

Marmara cencislate ce’ shciciaikt cocci dnlare aay eae lave Trenton shale

196

TWENTY-SECOND ANNUAL REPORT

MUSEUM ADDITIONS
SPECIMENS REGISTERED IN THE GENERAL

Sa
OBTAINED. Le
5o
NAME. 45
When. Whence. 58
Zan
July, 1891\Geol. Survey...|Conularia quadrata Walcott............22.-|.cceeeee =F
sf = .-2|Monotrypella subquadrata..- ...../.J5.2 ese... -eneoee -
Aug., 1891 3 ay Endoceras Sp. DNGeE-¢. J... 2052 ceee eee 7
“ 4 om ee eerie ts ) ORS 1
x As foe <= Sh Giada's Jode's 20 2. t See ee i
May, 1879 is --- |Orthis biforata Schlot.... 0...) cs seestebaten 2
Tie ncemeaen s vey Cheetetes petropolitanus Pander. ......... 2
eS ee AA os* | BUCARIA:, 2 bonne 50 -nactiedicce actbs ous oc teen 1
See Poon NS --|Asaphus megistus Locke.... ....... ....++-- 1
“A Bs ...|Cyclonema ventricosum Hall...... os vena dene 2
we csclenee en z .--|Chzetetes corticans Nich... ........ccccecsses 2
Seienae Toast es ---|(Murchisonia gracilis Hall.:. 2: .:...:.2s2.uee 1
= = ..-|Chaetetes delicatulus Nicholson ............]. ee te a
Soh oneeee ig .-.-|Chetetes mammulatus Ed. and H.......... 1
ccs tates - .--|Chetetes subpulchellus Nich. agate 1
o2 ...| Heterocrinus heterodactylus Halli...23 1
Boon woe eee ¥ . --|Cyclonemsa bilix|Oonrad~-- . seeeeoereneete 3
rey notes =e ...|Plearotomaria umbilicata Hall............. 2
fs .--|Bellerophon bilobatus Sow. ................: 3
er Fe i .-. |Cheetetes onealli James..........cccesscccecs 9
4 .-.-|Conchicolites corrugatus Nich.......... stab 2
Sie dsemenes es -|Ortonia minor Nich. ...25. 2.022 -2: Goose ee 1
ease : 34 .-. Orthoceras byrnesi Miller. . otros 1
= 25 ...|Lichenocrinus crateriformis Hall .......... 1
- - £ -. |Crinoid base}... 332.00 Pece,.os vwilecealan te see 2
4 7 t «» | OTEHOCeTaS:. 52220 the ccind. ae oe eee ome 1
eae - oe .-- Glyptocrinus decadactylus Hall....... oe 2
- - ze -|\Muarchisonia «2:8. 3% ots oeeecccc cee eee ee 2
Eetesttce ve ¢ Murchisonia bellicincta Hall................ 6
yobistsibin seater . -- |Zygospira head? Billi: >... 252s. seee cee meee 1
: rs -|Paleophyllum divaricans Nich ........... 3
: : % ...|Protarea vetusta eg 20 aid» clo este ol eee 2
Soe utee es os ---|Orthoceras . 5S Adie ite duaierdale'tnn cae 3
+2 & 3 ee minor Nich.. ,. 3:.00¢.s5. soe Bee 3
one color neiees Ea .|Dalmanites carleyi Meek................+-2- 1
hamesttcae eet 43 Constellaria antheloidea Hall.............- 4.
Geb eee nated ¥ -|Cyrtolites ornatus Conrad.............s..00: 3
Poe eon a -|Chztetes frondosus Bich 3 -7-*\t> ce 3
Mncbeoeusne 2 .|Chetetes rugosus Hall . a dus lesan eta 6
7 ae oe .|\Cheetetes fletcheri E. & H. 32a ceme ne 3
Be AL SOSA. re .|Pleurotomaria ohioensis.......-2..+...2+-+++ 1
. é -.|Stomatopora arachnoidea Hall.............- 1
. a .|Chzetetes approximatus Nicholson......... 7
Rap oenen wae Kg -|Chaetetes jamesi Nich..........6. s000c00e 000s 5 ity
ones ee eine 5 ..|Orthoceras dyeri Miller.....-.---.. Badd oc 1
Sy ..|Chetetes discoideus James................5- 1
: oe .|Chetetes clathratulus J. &N.......... eee 3
ances jane nas Zz ---|Cha:tetes gracilis James .... .....+,-+-++--0g 6
Br er oreeer $s .|Cheetetes dalei 8,’ & HH... "25. ccccuceus cepane 3
Selenite aicatae 244 .--| Heterocrinus simplex Hall......0........<.. 3
H esie she Ee E ee rp haat 1Gh. Baer di. Se. Seen See 1
Bests towns “ .|Calymene senaria i pag ep de 1
2 -|Raphistoma lenticulare namics ee - Sis Ag
tet He rcirctn gta ay .|Protarza vetusta Hall.. Pe ee - 1
“s -|Columnaria alveolata Gold...c.23sseteeee 2
Aug., ‘sot - Be ee irene (Billings.s: 22. 00s a cemcon cee eee pee coae
ype -|Thaleops ovatus Conrad...........2. 000-00 1
-seeeee|/DOxaster COMANCHESI,......---cceeee cocreees 1
Jan., ‘i804 Wm. Johnston.. Elephas primigenius (tooth).. Ae BS xf
as -|Geol: Survey...|Vanuxemia decipiens Ulv....................|.. - omen
Ae S < -|Ctenodonta socialis Ulr.. wee'v'e oe s\¢.s/s\e'e al Sta
aes S OAL W AT TE aac 5 ocr one tecnica SStiee wales

Tea See

Lower Tren-
ton limest. .

Cannon Falls, pun
Graf, Towa..:.....

r ;
“4 Be
STATE GEOLOGIST. 197
oe
7
PALEONTOLOGY.
MUSEUM SINCE THE LAST REPORT.
LOCALITY. Formation. COLLECTOR AND REMARKS.
Granger, case DPA deserve esis da Hud. Riv. gr..|Scofield and Schuchert.
Florence, Towa. Cincinnati gr.|Chas. Schuchert.
Neenah. Wis.........----. 2+ se-0++ Galena.. se “«
SI TMOSVALIO.) Wi1Se0...acic cece crinace L’w’r blueb’d| “ “
McGregor, Iowa..... ...........- Trentonshale| ‘* 6
6m. S. of Cannon Falls.........- Galena shale. |Scofield and Schuchert.
Mantorville. Mion. ............. Galena.. .|\Chas. Schuchert.
PRICIER LIS Onc oc ce cisio kis cciciceese Hudson River
it7
SSR AGS ra iatana cls <6 s'ai4 “soe 010 . oe Chas. Schuchert.
‘“ ‘ we “es “
Geom a | :
Cincinnati, co i ee - z: és i
“ ee olan ge | © ‘
OP lS Be Hudson River] - “ “
t» “s ** +s &
j x =o ina cake * i 53 g:
nate tee e ete e ee tenes ° ; a ‘
TUNERS CEG 6 cicc Shape SBCEEEG i + 5 =
nee tee tee eee tees ‘A zs a
’ CONS i Nd ea See at ze Cs fs sé
sete et eset te te eecees « ;; fF y
“ SG 0 ae a ere ‘
PWidVMeOSVINLE OF. 215.25 inne) ne wo: :
(OU 70641 OA re ae pean a earn Mi pe os os ms
Picea O te) Se Sopa cee Ps
°C ae ean fi ah ‘
Pa | . oe
Maat eens sete ee ee tee ; z
|) OMS RBar Sie C UOC ae) | i “A : ss
Ot sat eneecer tees sers m cy s ‘i
antennae eee e ene es . ‘ oa
nate te et ene tesa neces ; 5: p mi
beeen eee sees eeeeeees : 5 > #
: OxfOrd, Ow... esters ee eeee teste Cincinnati gr : He
Graf, Iowa.. G ‘ 6
MUI Ye seth wacea3 ie has ve :
Minneapolis, Mies LS Obs ote -lT’nt’nlimest.
DET ae Se Seen ea x ath Nelate mebieiee [from the Sioux river.
ibis roo) aig CLOVER SEN Bh apa ee Drift .j10 ft. below surface in gravel. 1000 ft.

C. L. Herrick.

Trenton sh’l's|E. O. Ulrich.
.|Hud. River gr|Chas. Schuchert.

7 ™ ‘oT: re Ls Astana >. 7 ‘
i aie At & - SS nas Sea ae
- “PR iw e : 4
i Y Te
mo
A hey
ya
gts .
ise
ae:
te >

x Y..

ADDITIONS TO THE LIBRARY SINCE THE a ee
REPORT FOR 1892. |

The present list consists of the additions made from Dee. 1, a
1898, to April 1, 1894. ;

A eae
Albany. Bull. State Museum, iii, No. 11, 1893. :
B

Baltimore. Amer. Chem. Jour., xv, 7-8, 1893; xvi, 1-2, 1894.
Johns Hopkins Univ. Circulars, xiii, 108-110, 1894.
Belfast. Report and Proc. Belfast Nat. Hist. and Philosophical Soc., ,
1892-1893. vig
Berkeley. Bull. Dept. Geology Univ. of Calif , i, pp. 72-160. Dec., 1893.
Berlin. Deutschen Geologischen Gesells. Zeitschrift, xlv, No. 2, 1893.
Bern. Mitth. Naturf. Gesells., Nos. 1279-1304, 1892.
Boston. Pruc. Boston Soc. Nat. Hist , xxvi, No. 1, 1892-93.
Braunschweig. Jahr. de Vereins fiir Naturwissenschaft, NOwed, 1889-50
and 1890-1891.

Cc
Cambridge. Appalachian Mountain Club, Appalachia, vii, No. 3, wens
1894. Register, 1894. ;
Peabody Acad. Science, Annual Reports, i-vi, 1869-1873. ae
Harvard College, Mus. Comp. Zool., Annual Rep. of Curator, ae oe

1892-93; Bull:, xxv, Nos. 5-6, 1894. Be see
Chicago. Univ. of Chicago. Jour. of Geology, i, Nos. 1-8, 1893; ii, Nos. —

1-2, 1894.
Cincinnati. Jour. Cincinnati Soc. Nat. Hist., xvi, Nos. 1-4, 1893-1894.

Darmstadt. Mitth. Geol. Landesanstalt zu Darmstadt, i, No. 1, 1893. a.
Denver. Colorado Sci. Soc., ext. from Proc., 1893-1894. ae

Des Moines. Annual Rep. Iowa Geol. Survey, 1892. tg
Dresden. Jahr. des Vereins f. Erdkunde, xxiii, 1893. Saf

E te

Edinburgh. Trans. Edinburgh Geol. Soc.. vi, No. 5, 1893. a
Proc. Royal Soc. Edinburgh, xix, 1891-92. aur?

STATE GEOLOGIST. 199

Glasgow. Proc. Philosophical Soc. of Glasglow, xxiv, 1892-1893.
Good Hope. American Antiquarian, xv, No. 6, 1893; xvi, Nos. 1-2, 1894. _
Gottingen. Konigl. Gesells. der Wissens. zu Gottingen, Nachrichten,

11-14, 1893.
Et
Heidelberg. Mitth. der Geol. Landesanstalt, I Erganzung zum I Bande,
1892.
I

Iowa City. Bull. Laboratories of Nat. Hist. State Univ., ii, No. 4, 1893.
K

Kiel. University, 88 pamphlets, mostly inaugural dissertations.
Naturw. Vereins fiir Schleswig-Holstein, Schriften, ii, No. 2, 1877;
vii, No. 2, 1891; x, No. 1, 1893.

Leipzig. Kong. Sach. der Wissenschaften zu Leipzig, Berichte, iv-vi,
math.-phys. Classe., 1893.
Liverpool. Proc. Geol. Soc. Liverpool, vii, No. 1, 1892-93.

Madison. Proc. Wisconsin State Historical Society, xxi-xxxiv, 1875-1887;
xli, 1893. ,

Meriden. Trans. Meriden Scientific Association, v, 1893.

Metz. Jahr. Vereins fiir Erdkunde zu Metz, xv, 1892-93.

Mexico. Memoires y Revista Sociedad Cientifica ‘‘ Antonio Alzate,” vii,
Nos. 1-6, 1893-1894.

Milwaukee. Trans. Wisconsin Acad. Sciences, ix, No. 2, 1892-93.

Minneapolis. Agr’] Experiment Station Bulletins, xxix-xxx, Dec., 1893.

American Geologist, xiii, 1-3, 1894.

Moscow. Societé Imp. des Naturalistes de Moscou, Bulletins 1-3, 1893.

Minchen. Bayerisches Industrie & -Gewerbeblatt, xxv, Nos. 48-52, 1893:
nos. 1-6, 1894.

New York. American Geog. Soc. Bulletin, xxv, No. 4, pt. 1, Dec., 1893.
Memoirs Amer. Mus. Nat. Hist., i, No. 1, 1893;
Bull. Amer. Mus. Nat. Hist., v, 1893.
Annals N. Y. Acad. Sci., ii, Nos. 1-2 and 4; also 4 odd Nos., 1884-
1885: viii, Nos. 1-3, 1893.
Trans. N. Y. Acad. Sci., i, Nos. 1-3, 5, 6-8, 1880-1881.
Nirnberg. Abhandlungen der Naturh. Gesell., x, No. 1, (Duplicate) 1892.

Ottawa. Catalogue of rocks at the Columbian Exposition, 1893,
Annual Rep. Geol. Sur. Canada, v, pts. 1-2, 1890-1891, with case of
maps.

‘ a. mp Re oe
200 TWENTY-SECOND ANNUAL REPORT aa
Way
=) 4 os
Puris. Soc. des Sci. Nat. de Ouest, Bulletin, iii, Nos. 2-3, 1893. ny FF.
Philadelphia. Tenny’s Geology for teachers. classes and private students, —

1871.
Proc. Acad. Nat. Sci., Ser. 3, xxiii, pt. 2, 1893; Journal, Ser. 2,
i-viii, 1847-1881. =a
American Naturalist, xxvii, Oct.-Dec., 1893; xxviii, Jan.-Mch., _
1894.

Rio de Janiero. Archivos Museo Nacional de Rio de Janeiro, viii, 1892.
S) ] Un ie
Sacramento. Annual Rep. State Mineralogist of California, xi, 1891-1892. Be
San Francisco. Proc. California Acad. of Sci., 2 Ser., iii, No. 2, 1893; oc- ag
casional papers, iv, 1893. i ?
‘Santiago. Actes de Société Scientifique du Chile, iii, Nos. 1-2, 1893.
St. Louis. Annual Report St. Louis Public Library, 1891-1892.
Stockholm. Handlingar der K. Svenska Vetenskaps-Akad., xiii-xvii, ©
Nos. 2-4, 1888-1892; xviii, Nos. 2-4, 1893; also xii, Nos. 2-4, 1887. ate
Abhandlingar zu Sveriges Geulaaisin Undersokning, Ser. C., ae Pe ;
112, 116-134, 1892-1893.

Tacoma. Proc. Tacoma Acad. Sci., Tacoma, Wash., ‘‘Is it Mt. Tacoma ae
or Rainer?” Hon. Jas. Wickersham. nity

Topeka. Trans. Kansas Acad. of Science, xiii, 1891-1892.

Toronto. Annual Rep. Canadian Institute, v, 1892-1893. —

Trans. Canadian Institute, iii, pts. 2, 6, 1893. * < >
U a WG
Upsala. Arsskrifpt Upsala Universitet, 1892. pets
Ww : Ff Rie

Washington. U.S. Nat’l Museum, Bulletin No. 45, 1893; Proc. U.S. Nat'l er
Museum, xvi, Nos. 950-958, 963, 965, 967-974, 1893. 4 ri
Smithsonian Report, 1891. ;

Z
Zurich. Naturf. Gesell. Neujahrsblatt, xcvi, 1894.

B.S BB

THE EXHIBIT OF THE SURVEY AT THE
COLUMBIAN EXPOSITION.

BY N. H. WINCHELL.

The Minnesota survey had no independent agency in the
State’s exhibit at the Columbian Exposition, but aided through
correspondence with the state board of managers in every way
that was feasible. The survey also prepared a series of typi-
cal rock samples, numbering 100, dressed to the usual museum
size of 3in. by 4 in., which were fully labelled and well shown
in a suitable vertical wall case, the various specimens being
secured in position by brass clamps screwed into the case so as
to hold both labels and specimens in position. This suite in-
cluded all the sedimentary formations, with some special
phases, and most of the crystalline rocks.

The survey also exhibited twenty unpublished maps designed
to show the physical features of the state. These were essen-
tially the same series of maps as those exhibited at the New
Orleans Industrial and Cotton Centennial Exposition at New
Orleans in 1884, but after damage by fire at Pillsbury hall
they had been redrawn, and in some particulars had been cor-
rected in accordance with later information. The judges who
examined the exhibits of the Mines and Mining building
awarded a diploma to this set of,rocks and maps. It is signed by
George H. Williams.

At the New Orleans Exposition the Minnesota survey had a
much larger exhibit. Whether any award was made for this ex-
hibit isnot known. That Exposition broke up in confusion,
the committee of awards did not make known its conclusions,
and the directors never carried out its determinations. The
Minnesota State Commissioner's report, covering a detailed re-

202 TWENTY-SECOND ANNUAL REPORT

port of the operations of the Minnesota survey, and of various
other departments of the state exhibit, was never published,
though filed with the governor.

At the Universal Exposition at Paris, in 1889, a set of the
publications of the survey was on exhibition and received a
bronze medal and a diploma.

In addition to the general award as above by the judges at
the Columbian Exposition, special diplomas were awarded to
Mr. Warren Upham and to Mr. Louis Ogaard for expert assis-
tance in the preparation of the survey exhibit.

After the close of the Exposition the Board of State Mana-
gers of the Columbian Exposition decided to dispose of the
State’s exhibit in the Mines and Mining building by depositing
it in the General Museum of the University, on condition that
it should be re-erected in Minneapolis in the same form as it
had at Chicago. This served as a nucleus about which were
gathered numerous other exhibits, donated by individuals and
by State Commissioners, the whole being designed to make a
large addition to the University Museum, especially illustrative
of economical geology. The whole collection, after shipment
to Minneapolis, was stored in the Colosseum building on the
University grounds, and was almost entirely ruined when the
building was destroyed recently by fire. Fortunately, however,
the above series of maps had been removed to Pillsbury hall
a short time before the conflagration.

STATE GEOLOGIST. 2038

INDEX.

Page

Aeurerupsives Of the Keweenawan ........0. 000.0 c ccc wees ceccleepecie 77
Actinolite magnetite schists.......... LPR IgE cite mi ncevclerceaveelg SI 159, 179
ACO UIOTOS 75) GND NTO ee re BP a ee ee aR ES 198
DNS CBIENTLS QUIN cscs vareersteyehat ore, o's 1d 01 share at Sea a aE Re omaha Icke 190
SERIE Maa 2 eo ca Lluis elaxclote 23, «5 << wares are Bee atewtoe. a6 idle agree laden 27
J OUUESID, GOUTUINU Gi epaare ORRARO COIS Clee 1h RPE aD Ped 19; 20, 26, 27, 29, 31
Pewee. 1TON-DEAriIng TOCKS:OL. ... i... ssc eces ee cetc ne weese edie oe 72, 169
RMI ESTAMI EDIT ULOMM EG fe parclesrai coh) afiyrerny ei covereretens oie) stream holes swet-saccra hte esd olecalapele sroved-als 19
Algonkian.......... abot shares abate ere GLANR a chsh ole elsi cade nes oracle Panes Dee eae 29
ME URE PANTO 95 op. erin 5 08 We oswlatn a6. sic, ww alae gale eNews, wa eaters 61, 62
(17) PLIES 2 9 5eYL0) (SIS 0h a a aa aires ee 21, 139, 148
SLEEP ELE <oB 8 UE sre Me eer ees a ee Ce 29, 122
MAVISTONSIOM ah eeprom a ee. |. ae ta Ce ate hte oe Ae eee 74
LS UTDULGS! TG Bae Peele ototcnig A ge cee Ray clea Ss ani Ry 4 ORDNE, ar Rl es a Re 73
1 LLPSUOUNS a WOU] RS 0) Cie CTR OO ROR Se ce ae * ee nen ee AE Re a 76
AMOS WCALIN OS INC HNDCEIOL Pee iae raters Sens saree Seto eae eee een 74
Pave beraa DUNT a MICO Bertsinys Siac 2 ee ons Eis fig ate w siotet ord Sn oes oh ate 73
NG KARTS SUC Wren esey ayer tena sie Pala what atm come teeta eis sme? Se nik BS cathe te 74
Anorthosytes of north shore of lake Superior...................... 174, 180
SE NOMENA TS SIP ss (Ree ORE Ao 3, eh ASIEN Tyo vaie wp ns a =p mae STS os els ee 17
Archean..... Sob Zid Atha eo ite o MEL nee pk AG Se See a nO ANT, Seca 26
outcrops in Aitkin and Cass counties Selene Stare Sains tac ihntctonls 26
UMMM TANI GCS <5. c0 feed ctv exes eens onde B24 scatoyfelatoreas aeebeatiGnster A © ele ene dsiaees 155
MMI MEAE ES.) 2a%s ec vss wae = siacccins 5 aa Peieate eeteae SIGS ere ac Aner ta ME 2

LSID 6 = 8%, Selge dae SA CRID Ie lore NORE eee Poe EL Ries AAA A me 19
J RCGC TED, LENOIR SYS ees es ieee Mee om Pre ol Seca es i ce a 17
PPE ASSIA AM VAKGH: 35.3... aioe t avis stolen vc erseecndbedeacs 22;
“STAT SOPRA pes SR et A A 73, 159, 163, 167, 169
Beaches of glacial lakes.. oe fon RI SIRCEO ees ee I oa tae 57
of the Glacial ne Aiconanin, SO EC AO SEE Re SOE RSA able 62

Gisbie Glacial Wake- "Warren... 5.3.2 li. aed. Neate 3! Parc eae 61
EeLhenyestern Superior Glacial lake... {sau . occ. ..c. os sca ene 61

Che 1, TITTY se AS IRN seal Coe ie ote ae ind Ae 143
PERE MENEACTIOS LCR sa cect Sate ce cee eRe eRO EE Hanis tobe. 61,6
ROW RE Sing Gir Ep cocnts SCO eee ey IETS a oe ee Gr ep Rey me Ai bs Econ 145

i SURV) 0) 26 A ae ee Seether ee Sea: atenes cetale tt eee TE 3
LS LIL ORS, aTER WG! CigbeP ie Olas ets i MARRS RU Sec I Sa at ee 61

Paice SIA MOvOt Lakes APASSIZ25..2ccc 8 oobi cloee Mec ude bel lds ovo meen 90,93

&,
204 TWENTY-SECOND ANNUAL REPORT
Page.
Berkey, OsP te os 8 a cae cn ie White f Oda Sine 1 oes ae 2, 3, 68
TEPOTE Of2 5205 ooo” Sako eke ois Oe tin a aan tinier taie = ie 134
Big Fork river... soc. on. 6 = 2 seve wis cae siasieie © oa sinss aielsle « 01s e Saal ee 32,42
Diory tes Of fo 242 oe nore cee ous tae wa den a 106
Big Stone county....... 02. .c.c cc enncet occ ce toes een ons ov ees epee 33
BITCH AK S syeic. otc sake Seeo. cS.» 08 Je a teeta eaters Poletelelo d+ ote ol Seer is shen 159
BeU WADA cook's soe took od ce 2 > Svs, cai ered ans See ane eee 3, 19, 44, 50
Boulder DES ssoss 2s oi ss ww ows See oe wine pees clei fe vied aps eee 112
transportation .0f 226... fee Leconte ane tid 2 aon onl 32
Boulevard beach. ....j-5...20. de. wees + ~ signe lols wim cfaele. © ocn!aletptb ie eee
Row Stritie river... -- << «0 seaebe se eek eee eis Cae Sree ae ee 32
Brainerd ok wos Fo tio eo wie ows 1 ee Ow wlald ele, sfs alekele doGisutele te sick oe ke 32
Brule” lake o5 Fess eo Pies nha ake alo vere ples eases alist ae eee 69,138
MOUNtAIN A: Lc. Fools Sethe hele Uae eels eee crete Oe «inxs ee eee 136
Brower, Jo Vi«.< sete. one onc vce net cline pean eek see ste =.) = 23
Burntsid@ lake. vax wi. «cite cs.< <2 ns tab teee oicte: «wise & erate ee = ol ts soe 23
Cc
@arel, Hy Oss nc Save one ee ene 20 eB ae ae + 4s opine ties pie ans es nga 96
PATIDOU, DORs «0 0 cic os oie cles <n cte whiple mele a deenein = ote el ne eats ee 134
Garlton - oar 2h eke na seb eee 19, 21, 34, 47
COUDHY 2a, - «hen a vain ae ale 0 aielntow efeln'e siege re nie vin ints i> hele 2
Garltonian .. «62 0.5 o> ei eee 2 «+ at toaje este ale» (helo wip leit <del sl 175
Garp Wakes: o.. 22.2 fesse Saneaas = Boe Rest tar Pe laste ce g.¢ + scale 22
Cass county......- OES eee een oe nk 19, 20, 26, 29, 31
Cavanaugh, N. J. 2... 6. cece cee eee eee ee eee cree eee ete eet e eee esceee 116,10
Cephalopods of the Lower Siluriau. -sca0 2.2008 on cles 0 ees 3
Chase, C..S% oo. yee See Sa reed ee coin oats he seine Sie aeons ae 51S
Ghester Creek beach. .... 2-22-2020 50 eee eee ne seco hee oho os ee 62
Cloquet river... 22.2... cece eee cece eee e cee cece ee cent ceee eens cnes tnes 31
TOUEC Si sce ase ied chads Sis, cos elute! o ehets ye fehene tele gots te ole ter teapot 145
Glinlis his Pave x Oa weed a own is Sie ena Rages > nian ener 1) ode eee 30
Columbian Exposition, exhibit of the Survey..................-...+- 201
Cook county, profiles aCrOSS...-..-+-- sees cece cece ee ete eee eee eres 138
Coutchiching rocks. ........2- ceceee nec r cece tree eee ee tener eeeeeaees T1, 123
GiretaCeOUS:. c+ = sant ote = sat olen owners orersieite sie ele = aaa eee 26, 99, 122
ridges ......- wien | oa Bole eee oe De soe ae Cah, pena rE ce oa 100
under the drifts. 462 -. «0+. ou tne ease meet pee oe sete ee oe 29
Crow Wing County........-- see e eee cere eee eee eee es 19, 20, 26, 31
GulverpG. Bisse sos Fhe kage oesig eels > te te on ohne ns an 2, 36, 49, 50
notes on the geology of Itasca county.....-- ..-+ sees seeeee 97
ID
Dam lake. 2. - iain. oe ce peek oo vee oe one ee wales alate ee opiate eae 27, 28
Dawson, G. M....--.e ce ceee cece ee eee ett ete e ete t terse eter seen ecees 37
Dawson, S. J. ..... ee cece cece eect cee nce tee eens neeeceten cere geeees ces 22
Deer rviver...-..cccecr rere sees ce cree cons cccacinas cwmaele sac er cel Sain miele 42
Deflection of glacial Currents: . « ; oh ..0 bea Pei ae eee aes 41
Deltas in glacial lakes.......-. 2252s sees sree ee cree eee eee eee eres nee 64
Diabase in Aitkin COUNTY... 0... eee cece cece cee ee ee eet ee terete eens 27
in the Animikie.. By. 2... ieee ee we eee ent eae 6 elle eletle ates 7
in Lake County. 2... ss. -j4s noes eelg ete tele tots « nines mo 173, 179
49

Diamond iron mMine...... 0... eee ee cece eee cece ee cence ence eres

UO Qae ce

STATE GEOLOGIST. 205

Page
MES U LE SILT, Ester OT Kita pox, PIRI S ciaqine, o akeisce's's ode sotelva Ad\eeide veers 106
OE WO GOCH VS BIS st ececs os x He «aisle o's oes o biv'e te emieGaia te ou ere 107
PCM E Nee Es DV DCACH isco kerctretscciesatese soe Sel ature oles svetlo-s steve ove suejacere eee eels Soe 61
RES Ere PEA CL Gal cscs cik 5) cheasig va orarciatevn fateh aleve leleye six a laiesave ld e's ave Wen eyehahe eteis Subene le Gases 122
MEPALHOM Dy WWalnenwUpPhaln,..22 25.05. cscs neem eee mee 18
DMT CKIMESS!O ltprereg race sieletere sy5 10-10 ales: s csavopcudehe So a elena Ma ere 20
MBPEICSSIS OUST a rrraie cyarclooreiale oterhe oiaierere als. ejere'e-dicja.e sha\eie aa Sota oa aarti see 124
(Lins BU 22 ae, PS ane rae 19, 21, 34, 41, 42, 44, 47, 57
HVS A GIGS pepe rorete oietan cyclase) asiisas «carcass © Shad; Sravels cides eave gh alee sve slave th Seaeleioeyawe 61
E
PEAAOMMNC TESOUEGeES Of ake GOUNLY. 2222s. osc ebos ceewens dew degaens 146
EP ON esd 5 asd Seed op cad t sessed omeaceag 2, 23, 24, 49, 50, 52, 53
MFG UEO Leste ont arate afatcrale o's, «. 6 ded sisia’ Soe Ger Oe Hed at 141
ROGkISAmMples.COlleGtea: DY. ;.24 -2e was ee wise ces tice Soe eee 181
ME se fer oh). fob cs oa ce pain Sinan’ nine ant digas Sie lapeediagale 6% i case's some 19,51
MOMMIES alee os co: eal Oe ee ts crt ib. clas aie drere seater Deis eisiele oct o a mieten ere 144
RUM MRO SEIT CHMLOVETMMEMUS. «5 cerailcictes <> sss ome ore sha sirecayelee Sisieisberas ecto aes 57
ME BEI Pict Po aca che et ch PMI oe 6a. Koos siaiata PRCA eater w Me Sue aT 53
Exposures of bed rock north of Red lake SRS ie on ote Ores Aor Ao niG 95
paeAa Melt BHC CASS COUN LICS <2 2.0/0 Sree cess fet ds aoe e wibelere 26, 27
Exhibit of the Survey at the Columbian Exposition.................. 201
F
BE ML SISLINUANTLE 5 cla cfd agicta state viene « itjoleia a Oc a uate diega cen char 45
1 Et) TDI a Ye ACH Dh eae hea ce em eT A oe 61
Sremrereratte SWOT SELUITIAM!s » c(i viz 2) 7 Rs ca eiak ces cso Be aw een cab.
G
Pea PHM VORA NNEC as covers ioeieeca ees ci AcS arcs aie oars eledels S Oak oles eR c vii
UIE CPCB) are peaetacinn hie eles oN cee tee ote sale Oa Pe ae 169, 179
PIG B eter ase) ters jarsie 2% siele e ejojeveccle alate, Sie male 6, UA PRR ere ER Ae ene 76
PemmammerdsyO1 hire OWE IIIA: <6 x. fo. Lecce sacs codes ceca cece 3
eats ROME RIED INNO rere ce fei sate ceeysleV ote tovesd endo cee heroic 2 Bh ite wo onee Feed dee wuebns Pe Bill, ass
UAC g Olcreystane oy cho seep eter Selaareg Ce aieraie etnies ok sicko waeeaere Bae 8 SA Be 129
REE Pte oe ceiaraie fe Bae cla oe «2 aloern Wik coos SD eee os Stead wales 5163
BeMPEAUCHELCIIUS, CEHCCUIONS Of... sve occ ca lawcs clea s eee dudesccsvcneun 41
SUNGN aA ihe tM var eer css Pata Cao cln ead apels aldbatets & a vicne vedere yes 31, 122
FeOGEMOm by Warren, UO PRAM occ. rs oes scone melee bs Sevens 18
FU GLSTECSSE MCSE SPS ee A A a es ei A en en PP 31
SUB Sue Ge oe 6 UB an SAS re ne OTe CRITIC EE oT I oa eases em 34, 113
PMNMRETECRTAR SS) or 2 2 Fe85 Do i Moie arerds cic tyne owe be eave RE EM se fordexake Sate ete 3, 50
MPL RBRA Rees Pete e, Sete eet ota Sacre a atin cco oii As cure wie eae ise 49
MEME EEL Crs oh ss, Sew tve ee ticcld « eervin dare See oS 6 Ok sieisinde wee Oaks 155
CLUBULVE ie VUES Ole <a) sitet statins evetd'ss oes Bees bate e 71, 118, 154
EDEMA ARTES DIDO 5 ooh Rieke aie ieee atare orcale wie ateCemin ves So We helak 119
Sem ReC IM Mle ns aye La. icy 4 5 aera ag cis ecole Weare a ourebines 70
SP a ELC LE KPO os Oo cla Out wo, wins Seba we gle tees 155
Grant. U. S..... SOF ER eo BE eee 2, 4, 23, 24, 36, 87; 118, 134, 151, 156, 157
FRE] DONE TO) een CAA cB Greer MRI Ain OECTA COA © anne niet eer 67
POG SAMIBICA COMBCHER DY sid oc ome sitceu, clones ss Soule ead ele 79

BaRGatee Ai SG COp cect tea eRe ae os oc oe Maroons Sa lout ete otne de mes af

206 TWENTY-SECOND ANNUAL REPORT
Page.
Green; BeBe. ta sek eas Men es eee ele les dabecy oe Soe eee ae 116
GTreenstOnesirie eas eee echoes vee Saep ae ss Hee eee ae eee 108
Greenwood: 1aKe22 322 525.5 erase sot oc «so aerate ene Sd eae 143, 170
WIOUMGAING <5 222, 1ct ae See eee» Stes Sel ncie Soe ese ae eee 143, 170
Gunflint lake..... Silstesids wey wo Guiwe she's © ine bso aces nigel a 22, 73
ANIMIKC: Of 55:5 ess No carsales cieit nie ot) oidiea co dic: e sled Sineaee sje eye 73
H
A GOW saint gee oc he kate see aoc cae Ste nie eo ee ee 150, 158
ET TA WAU oes oie 3 Sinks See 5 ote ele Geico a alu: v clele ebajericls <fe Sota Sear 20
HMibbing.. «225 >.2 Dh aits ch ee duce wid's Si oelaleie yp emcee 6 eee = oa ee ee 49, 50
Highest point in Minmesoteic.. 0.5 20. on cvises ce vlna ss occ 0 os etvis nee 3, 135
PR IANG el cha sus wel ee eee as oe abn oe oa cle cate wee ee 44, 48
TO UL o/s, :cteve Selec a hlc 018 ae w nlete sere tere a Sonne eeu oleae a een 145
Honnold W.-H ease ico. Ton wh: aie wattle title oat teas: aco ae ois 166
HIGlyOke!. 22 ob co tance ao Sbtinesc\ wees Can wely sh pene tae eae arn 19, 47
Hovland HB ..os.c.. oa bece Sak eens Acie a eee Le eee 90, 91
Hubbard :County «1.0... -.0:6.6.5% sicareatelen ove «ieee oie Seen ee ae a 19
I
International Doundary...< 6.23 decd ss dvens Secs se ee oe eee 3, 138
MIVine der Dates. aes atasiea es Ro eee ne ee ae 73, 77,121, 161 168, 170, 172-175
TSapeulesvivers co. o:.% sie eee ee ee So ee Omacee Seen Be eer! 50, 149
Mele Royale .os... oo ds oe i th eee ee Se ee wl iced eee 33
Itasca county, notes on the geology of, by G. E. Culver............... 97
TGASCA MOLAIME 224 5 65 ob nisidisine ge wlvle cl Uoiciw las Bal = wie tras nee Beto 49
J
Johnson, Archibald...... OE Es eS ‘saat 30
JONNSON BWP. Sec Aca ce tw esd oho a ne ee eee 116, 118
K
WOAINCS ob Sec’ aes s Svidis lors Valse ee aie se eM ce ee eee ee eee oto ee 53
Keewatin, rocks ¢sce0 5.4062 b.0 bode cle nip tein oe eee eae eee 70, 120
KCWCONAWAN 6 oo ook s 6 hctse Heine vere e's o\n whl apie fae eee se open 29, 76
acid eruptives Of 2:..:..c0 2 on. Sone ase ae cael 10) eee 77
ANOTEHOSY ES OF -..6 1 oe. 2 wieis wnperctelse were s ve Cee sees ee 174:
diabases Of). 5.6 2: é.la Pies bb ie glee Res eae eee ee 173
PADBVO OL. 215 o ic. ics sew cise co Aureieiee «atevers tea ele See 76, 169
TEGLTOCK OF. 25.2 5 5 bcos oc sss one breerew sicruks Coke > eel eee 170 —
KSI DOTLY <5\0i0:5ics,2 saa aioe ceo oie" aca Maistose oath eloeiers a halo’ = aittete ett ho 27, 46
Mmiiie- IaRO so on..joc' oot io oR odode ores vases wees Sane pele ieee en 22
Koochiching falis.is «.. 025205. < fo oss 3 efevepee oe tees ee nee 101
dioryte ate. .. fesse des oe Casig@vegie seer er see ene enn 107
L
Dake Agassiz... s.c22.5. <. cuact then ¢ auwie eee peiieoeceis sane ee sean aan 42, 52
Lake: Algonquin. -2.0°05 2..fi.' Desc os. seslepte eee he Set os Re oe 54
Bake COUnty sc. 8b A ceo sgt bag vos oc alecad ee sae ene eae ee 143
€CODOMIG TESOUTCES Of 3.2. os enaae nae eee oie oe ees Penne Dae 146
map of west. central partiof . .0%- 2. tcieaseesesiem sce er eee 150
FOUWGCES: Of FLAVEL TNR so 0:5) sm «shale reicys ahaa eit sxe oe ele ote eye 143
TOPOLTAPDY, OL ses cc accticre raced os epeteseoieis «Sn cael tole ere ee 146
bake: Harriet... c.0 of fan's cas tude oknk tpt beck vee ae 50

STATE GEOLOGIST. 20%

Page.
LLP IRS GY? GINGA WOO aes aeeroreso on Doron Erne Dok enn Santa tina toc 42, 95
ee AU RP AIS tala Yororre ele, ip Bia alee RSIS) a mimesis Geis a tela raltvelavele'ed TeRhrarerel he 31, 38, 42
ANOLUMOSVGESLO Lect apace stansteiescl ayn sha siale a. s.ecersl ola gaieaveis) rane biaiate easy slaveele 17
RI UKMVV RTL OT arses cree iar aah ale le ete iene) aTarcno aie ore bw araoie alsa elele Sermele teenie ese 54
MERE MEN VE PIT LTE Soren Nelolanie ones tis ite k-ate ms x nla alesse seas algdly ale wie ener ae 42
ijamellibranchiata-of the Lower Silurian... . 2... 6... .000 ccs scene eines 3
Mawson; As C2. eteusiens 29, 37, 55-57, 60, 63, 71, 77, 96, 107, 109, 174, 175, 180
Ree eae HI SRM Ne tee eevee Cs ween ee secon pavaieree Cie cavctanors Arlene eee iaieteaeiaiowesaners 47
LsBEOT IGRI a AOS Seas eis a ae Tin ar a ere ae Paras MSonron a la, Soa Ne 52
memelling-parby, report of, by C. P. Berkey..)...... 2.2. .ece ce cosneae Bae 134
Coe VEE ig URCHIN as Si ee IRA PI i 56
NE PRUNE UE HLTA Pyros, <x yt Sei nis Siwtgg fin. cela, sip Doro owe Uae Gu vib bape & aS wens 198
> PE. a RS CSR RAR oa ne OS abe PGE Neh 30
eam MN ERD PETIA s, cee <\ ois’ = Sisceieis ete-s’ « o1c's ws uh $late. See ainin's Dh sje we elne Hepes 28
ARV ETA SLUM ATIELOSSUL Se i<s. eta sere snc. cis ope ake isis Utena eas wan ble oes aes 3
nm
manomwest central part of Lake county. .......%2. jocce ces cece ene cs 150
Map of the glacial geology of northern Minnesota.................... 19
MORGANE Ale N PRIN OS wraitctch eval tisiaho] evel ele vevdiaicisteltevce 's % avai stat oiels wictaleitiese ome wpe iaichsie. srouczeree 136
McEwen beach......... 5 an BG SRE Re ATCase ere eere ee RE lotic 61
rE CLCAIOIIGNT. SOS eric Eee CIRCE ico aE ee ET ore RS Sera aie SR Rare Pie 3
RMAC TO bao coe Dh acs sc ns a clans poeta 2, 48, 160, 167, 173
ROCKASAIMPLES COLE TOM Viera trees! stercro elatecsietsta/ae elas Seesteteteyal uel sfavesete 87
i STREET 1] BA 8 IM Se a ae eee SES se 142
LILES ETE SIT ACTA Bre SAS Oeics keel Aen es) Bcee ame mne Se 2,50
TESS ONL DONOR AER AS es ae PAS piel ane ins nip aS Se a erent Gre Ear ae (ea er 50
TOTES <a GS SARE G ert COCR aOr 5 hha SNS Saved ne co ieee ONGES 28, 29, 31, 33
HON odle sols Ceres p OBS OD OSE eC SORA OC r ee PiACne a0 oot omen 145
SSE TN gO Mereteys seer ctsteces fata os ete) ich wis, ates a e/ese¥e-ofsu ht saute, gvoh miehe (ate svete Gisievens 2
Niles CHISESEOle lbASCA, COUMUY .)..nc nas 6 4 achieie ciao! tetekeon clove sun e.e46 alae rte ete De 119
ALOIS: TOBE ASS AG eg Se it, ARS NIN) SSE NERE MRNAS OPS OESS HE denrereta ar yee EEE aa eT 46
PME DUDEM Nae es ey cya obs PS cc lala Pst cto! Ghal se cue) le SSE sea wares elas 32, 44
POMBE DT APART Serene ttre Seo fatay cate tvato: sinter oun ois at sis Sioiereitieittererare skewers ee aceon erere ais 3, 135
Seen DTN OT foe inches gS) ia aoc tidie > shies aR Sis loiwieleie eiataiels ats 20, 23, 2
SADT NEC) CHANTER SE SAS gor tee toa Meno Pec tas ara ips teers cy AR cine eect ae 52
TL USSh JEL BE GO ROOM 2 ap foc Gear ee er AO he nea ran Age eee re” 19
WMOTAINGS: 25.4 s000 0.5%. Weare Nae mi eens ASS. bad Sah 31, 93-95, 111
GHG Gall eateye ott arenes here talonel en ieiele dicielare e's slieie oratoewis aie tee Geis lbers 45
EDI ITE OTL, VATE i a8 ah Ble BI ty ne te Sa SIE ERIE ies eae ar ae ae 134
(0 AES 2 ETT Pa oak ete RS SE na cen re ne eee ae 19
TOL CEEVEED s 916 o Siete ie aU 7 RR 8 ta a ea 26
PMMMBURTIURGR EN TLED IT CP oe 55r2 s slalsi vetoes erate ea see AOR ene Roar ee Llane tas ee ay aie Sy
2 TEED CE CACTUS TPS 2 NRE RI eo ne ao 190
SM REI ah Ve NAA o-Ps fe eTocs elas sbcecei a Shee 9, Sip eivlacelalsiaielbin ou 28 sy bak 123
N
Ee MEPMML ETNA re ye rar. Seat sie c ne, a OM ace Te OE Oe 61
ee iT re eet it NL cat ce a URS p Lta Sea eis aianetaie kien ale ide Fle aie 31
PERE RUN CITGEES rove UY 3 isla Mash preteens At loc asta cates oa crmetelve malvtts Saba lcaltwen 64

IS MOEA ogo ou OD EES Wife tenes ra dca cuaate, @ BLs miei wtereinkelarnteroned ote: Stele. Aarons 29

- * oe ac
208 TWENTY-SECOND ANNUAL REPORT
Page
WNunibers 1786-1968), 20.0%: :c6,. do. 5 vivo ake seo oo siecle SR eaaeea tee eee 5-17
PRA2Z58 Mis 5 2c 6 2 gba <(Sereele Sate bol ehnis’ a's en's eta’ oe Cane 181-189
BOLG~1OUGG: 0.2). ste dawie voiciat ane eae sie, oi cjale aaa ee 79-86
1B 3. ER OS ne o aieis-eldleseis’aye wie. 4,0 oat ale @ ayaa 9a} 87-89
IS=2908 wc Head Tonge Ste Ate ae ek oe oa Seles veo eee 125-133
O
OBrien, I. Cad ss wk Selaats sip Cares abe plomalag Paes oo tik ee ee 90,96
Oyaard cA. sic onrs sea chguens oe ee ct see oe ees 3, 22-24, 68, 69, 134
Ogishke conglomerate. . 2.2 i0Seecc 00. cays fetes dc solb sos eB 70
Giter-Pail- county s2%:5... 8. aoe deeene monte ale Set clals e-s'a.» Daina 33
Ottertrack Jakes. . ysis. ..csthek st\lenee oe a aces 2 ee 70
Ostracoda of the Lower Silurian... ot 2.2)... 2c nae oc csle tae eee 3
P
Paleontology of the Lower Silurian....02 2... ...%. dens sete. +. 2 eee 3
‘Papers by the geological gorps., :22..45 Gan. '<\ssene eee oso ee eee 4
Pelican Taked cg sc 5 eis vic.s z.» cadens Wiate ka erates eit eke ot a 31
Eewabic quavbzytess'. >. 2.0% oc oVawmiticenes an eaerreniee 28, 74, 75, 102, 159, 160
Pigeon point. 22.03... . «sa age’ 0 eid 62m ajehe| oils aVoray'sinves \asel's. Qpeialhe eveToR nance rae oe eae ean 49
PAVING. 5 She ist cloreic ees 50 ado "eam wis ote so Rivne sn aad a 0 ee 53
Pokegamia falisii::.. 60.6. 2 sce jens terete Ore etuleve » ares oie eases ite oe 28
QUBLGZY Co arias ag os,rcters'e leper elaleterele ays & cle ie «uote Dene oie pice eee 102
Prairie river ‘granite. ..ies'ss e's ccm tee Gs oe Seis dae ee ee 105
SLTALIZTAPDY Ati s aieieis si. on, <eic'nislaeies > bieles olay Dale eek 105
Pre-glagial ridges (Cretaceous). 2s) <<). sc.00ce pe cleticclovy ose eee ee 100
Profiles:across Cook COUNLYs .c..0 icra hes c «sions oles. dre eee aoe ere ats:
Q
Quartzyte, and diabase in Aitkin county...............csccccccevccece 27
PEWSDIG.S. Ni Siw ches criateeioe oye ees eee oes 28, 74, 75, 102, 159, 160
POK ELAM AM isles. 5 Sic dialet wleiare Cieheccieteteoial ates elena niente el Cee 102
Wauswaugoning. ojo. )s sane atic t'c 08, at > leleiee setenv elas ane 75
R
FRA DDI b TOKO woo sisiogl ooops w gue viet n « olate imine et tetile lagevat ais Bier eto tnetie ete 28
RAIN Ys WaKe 7... nieeetteind eae Pa Seok See onacuon ors so: 31, 32. 42
Breed Wake ©... Atlacis So ste ween egies v amadlate sceithneshlea's Classe wie Seniesa eee 23, 92
REO STIVET Ss 2 0are sty .ois bisa ho acd stele: oftle’ «ose vayavaio kay kein cle eres yoke ote ieee 34
BRCU BOC Kiso taiedate scree Mee oie eect RN Pe A ee 2) 3, 11, Lies
PLEO WOOG: Wallac 3. Sa cc He Baie eeoiate ete hale oo hetero nocueneh ot aubnoiOes ee toe 30
Reportof GC, Py Berkey sjc-ciis vjacie ee hs dc Sune sat ee 5 selsteiclaydalen Ont a ee 134
GBA Culver ne eae ahace ene Seles ote breeilelocte nieke sh eae 96
AS Ee POLE ta Fst oe iefehis.s Slase.s aby. epee renggetele ya os eter ete, en 141
UWE SM GTA tens Jie bes 5 cite din So diavapaie rele tai ety oral sel re cai 67
J> He Spurn cst. ics ds Jest eke akeSlecets Salome sce ere ean 115
J HE TOD ais os sccicgiceeige + ove b.8 <a are onseia tease he) paca te eee 90
Warren: O phranns corte. «oe. oc ae etki es once 8 oe lea hate ter eaten 18
Retreatal Moral Messe orsso) oye She aes cares, oleae eee ee ae ate ode 45
Ridgeway beach. . ./23.4 5. qs s Siete bclers oo. soo dn ips wl aieie ota clone nrctet een 61
UY OLY:GES +: sh. Soave oo sesapeis: nciorscore ooo) ayclale ietoicns oe lhals sis te nie ante Sutieitets aan tate 77
Rock: numbers 17 86=1968 5 MN ie isso ile twrsaiersyse. cyetews ole pplclolovel states deateyets i ateeaaee 5-17
1288 Bu oes os aro an oot silts ao era ia eae labia eee 181-189
804 G——1OIG: Gs Biss ciccs «bio e diais se ic pa atcatahar. We ORhas poets Male aneneee eae 79-86

STATE GEOLOGIST. 209

Page

EEE CAN | BNR ERS POR a rai selec ae oe AeS PTA ene enn Se NCS 87-89

Be Si cereta Ae eee oe EN ri Seas Pe ek ene era ee BE 125-133

mock Samples collected by. A. H. Elffman.: 2... cis ee eee 181

NE DOM AO I Ae be aby Gee eee aan EPs ye ee 7

LWISISIALG IW oN amet ome core Se Loe ae ARR WeBt ar EIN choco Eco 2 79

Meet SPUEE cee ey tc sche creel + Br me at eae Bo 125

ENE iT LG Te il caes tan seis tacks. Seals siin's 'e-egesave Ae capes Spee eras ole 5

aE GES RO LatTeh Vie loli sls AEN COULTNGYs 22 ceerans «iors wneeuacwiefs ans siete 1s cWe raya lenehe Noveyatel atenays 143
S

Rae ReA MET ANT oo atei MES actos faye! ces Sis c0N6 asm os SiS tow Kislata/e aia ois sahoge ave mse ane ete 70, 71

RMMPMRMESSIVG TION PANES. nce arceleset Bia tesa sie & woe Dans eadie wets estes Unie mae ae 35

Pe mmm RULS AT LST eK ar cte ictee tw oes e's 4 ho wide Dems ates DiRhe eda Pegeleters eh Penags 20, 31

GRUUDCs ORs. ais toe Sere Sw gFk he wren cteate. slate ave cee ahaha nite alate 145

Se Oible TREE Soi. oS RSet HSI oc eee eho Chee Aen om eto 34, 44

SE RTI SNE te FSR a eS NE Meer: 30, 48

maAIET LEED WOACI:, one eens «62 ba Sieben ® panic aie a ea de a eure ae 61

SS, OH THES GANTEUICET WU Fe A So Ie oe ater Ai cS Shen) 8 en ice 76

SE TTOSSTIS Of LiOGWEra ete te x. os wis hoa ae oe mayen ids yous eal amie 3

SES, ENOMSON 2... 5 os etic oe es Pere et Ae iy pee Pre tent re 121

SEMRTEVINN MT CAIEN, (Cot 50405. c)=1 o.oo cls ioe, x «wig ANE ote Maat wore taus sO ate 37

SAE HERES MIST VIE Taare PS Spy cone eS NE ioe eee cs eta a Se ahs Lane a edage ota clate apa erotave 26

PMO AI KS LAKCI SS oats ileste cede s oa 5 eM A ok We abaya Nana sen eee eo ole We)

GATING OMe ate cc Stee: otare ote Stet» « PS honeur\aSel nee etale epeiele Flos Me oe) 155

eM IED MCAS EMA INIT A ec rer SS cree cist er ctetindes when idl habe atalc muckepaiaaIN ty Theses Ws-tt arabe 96

apMETBINCE TNE ere So as gh etseac Sfio. cc's ays «Sm wit Beare Clie he sh alate ee cellalb tote lan ste ave 59, 60, 62

LE Ge) 000) 1 Bees nO he Re a ee 179

PORCINE ieee Solan tah clctaete meine si oe ak eee a etlsnnys eis 2-4. 48. 54, 11, 12, 74, 121

ME [OOM UO Nise eee mere eer eae Rae Sale) wap abel ewsts, Suataiean ole ake OER setts 115

MOCKS ANAND ES TCOMLEG COME) tess sie leteiers: slaiela chara niewerste lots ste) eleerels) sis 125

SHOEI COTDINU agee ieee te oe case Se eee en Pole Pe ae iets OA oer Sie ae peat ea 34

2. 107 (SCV ES 2 4 RSPAS Se eee ee a C8 MS ter ee AAS

EA RPMERIVMMTOISVIC Trees eie ctor. ois 27 cto arietcn earth a nese! tic nae g ndeias Snel Prace ore tt ensayo ha 142, 144, 148

yD Oeeyreens ees ears ars aiie sein Seems sisi ayer, Menai alors cdaiarie nate Mine atu etanete 22

SSRECEMINE AUIS te) ETAL set. te tanec weatlnk-uultcdeicteebaie aleimiamnialle ois oa ese he eiecete se atey 1

MMI Te tee ee A ds See Pa es eckns os aera ccs iste oun vid GE yarAe Sikes DRO Stee 20

EMS O RAN IGUMCS). 000 acc ns os sensu s opens Keeesceae riers a4 21, 139, 148

1 2 bo SSE ARGS 5 OREO SINS iglesias oles inna Mime Paneni oc 26

TREO LY BAB Soe ae Geese ory Oe ho Ree aM eee Pana ba inne eee en 59-61, 64

PM UMMC AC Mma: taht eR OAS ar ain Som cia ete hols Gus stove eclelcie a2 epaie Cia sietiote 61

JU LOTR IEOM as oS Rage Ere S DOOR no mene APRS MeL reiiican eer A aes Pee aa

DBCS tear tetare erates cic hierar ont Lov pyay ee ee ctcooRTs nis els sets Pe Ge eerie Brea 121

SR rene PGE Te oe. SAR te nt elec. SEAN Ane HORMEL. hue eetow Mee 43, 111

‘Litnthal, do [Blab cast taen ton Ge crt eerie te Se eo RACICR eee Rear 16 eh oar earn er ee 2,19

FHS] QOL. gs Bets lees RICE OE tell Oana Cee RN ener SPC RE 90

rere y Ot PtASCA; COUMGY o.: uses ieee es sys die cis wablne cok /moleb alee 2, 98

of northern Minnesota, methad of work.............. ee, eS

of Lake county..... 1 a A aA Sate et ae PMG SP 146

TEE o bod SRB ae B Boa ASS TINE een 2 oS tee EN NER Ei i ane a tea 19, 51

AMON PALO OL UO OUWMLCTS. 3 f.>. naa bee atls Se Suet ue le Se Se Dee ain ole 31

a # BRD is Ss >: As. % Bee 7 . rf) Bee d 7 i a earn aah
2 re eyes
: , Baa
210 TWENTY SECOND ANNUAL REPORT | ha
‘s Page
Proat sakes... oo 5. 6 Sage c oe ip eee fe eee ee ee ee 2
A Wo FEACWOES ioe oak Sok ck Dead oso on eo a ee 19, 47
el i ie TiO Ree ee "14528
S
WULEHCDS TE: Osos eric cs pe St cre etna A ers eo a ei oie
iphone: Warren... fo. b.ao2. 3 sae eases oeeak ese 2, 4, 317; 938; 147
TODO Whos aSek she's ese ©, cote AVES eee atetettie sa oie RE ee ate
¥ ¢ |
Walley drifts oi sol Jac! 3 ee eee eee -Saeae a
WanvTise, Cl Rai. ese cscs susie 2 ee oe oe ene eis. ene eee 161, 168 ; ot
Vermilion lake........... TAs a eee eee) 2 en 19, 23, 31 a
MNOT ARNG o50' 3. Say a gaan eae eee a ee ee eee one) ee
* rocks, same as Keewatin. 2... /.- 0. - 20s dvcnee-. 0 <0 09 eee
Wireless sed <b seiccs aso. See I ee ee ee |) od ee es
Ww }
Wauswangonine quartzyte—< 2%: SB eee ee ee Rare
Western Superior Glacial lake................ Spt FOU ae ane arabe
WieSt SUPEPIOL +2. 20 ose soe. 1 out Wales Ra Steshs Soo" cas ier te: are aa i ea
Wihite; O2cA sacri cies Co eS Garces nes Sees eee ee ee
Wibite Ohaus tot ee, oA eee eee Cel nee 142, 143
Wititteface TiVeD 2. 0os. = nbs noc ee Rees eee eS ate |
Whittlesey, Charles................ Leah ES pea eee .
Winchell 3. oo) a. c ese e ee Blea Se ey Se LS nn Oe Get a
Wiirichell,-A. N=:,. .,.vcc07 oho seeueen tee ee eee 22, 68, 69, 134
Wainehell He Veo oi racen ek 4, 29,36, 50, 68, 71, 74, 96, 98, 100, 122, 160, 162
Winchell, N. H..4, 23, 24, 29, 35, 61,67, 68, 71, 72, 150, 158, 160, 166, 167, 175, 176
exhibit of the survey at the Columbian Exposition........... >
rock samples collected: by... 2)... bates ete oe ee
Winnebagoshish lake......... “sis be.0 seeks hi tee cea eee “he 7 32a
Wright, Go ios. asc Wo cle t aun ve ues Sk aie.c patneiekts Se tee ee ip par ay.
'

PUBLICATIONS OF THE GEOLOGICAL AND NATURAL
HISTORY SURVEY OF MINNESOTA.

I. ANNUAL REPORTS.

(Distributed by the State Geologist.)

THE FrrstT ANNUAL REPORT, FOR 1872. 112 pp., 8vo.; with a colored map
of the state. By N. H. Winchell. Published in the Regents’ Report
for 1872; contains a sketch of the geology of the state, as then known,
and a list of earlier reports. Second edition (1884) identical.

THE SECOND ANNUAL REPORT, FOR 1873. ‘145 pp., 8vo.: with illustra-
tions. By N. H. Winchell and S. F. Peckham. Published in the Re-
gents’ Report for 1873. Second edition (1893) identical.

THE THIRD ANNUAL REPORT, FOR 1874. 42 pp., 8vo,; with two county
maps. By N. H. Winchell. Published in the Regents’ Report for
1874. Second edition (1894) identical.

THE FOURTH ANNUAL REPORT, FOR 1875. 162 pp., 8vo.; with four
county maps and a number of other illustrations. By NV. H. Winchell,
assisted by M. W. Harrington. Also in the Regents’ Report for 1875.
Out of print.

THE FIFTH ANNUAL REPORT, FOR 1876. 248 pp., 8vo.; four colored
maps and several other illustrations. By N. H. Winchell; with re-
ports on Chemistry, by S. F. Peckham; Ornithology, by P. L. Hatch;
Entomology, by Allen Whitman; and on Fungi, by dA. E. Johnson.
Also in the Regents’ Report for 1876. Out of print.

THE SIXTH ANNUAL REPORT, FOR 1877. 226 pp., 8vo.; three geological
maps and several other illustrations. By N. H. Winchell; with reports
on Chemical analyses, by S. F. Peckham: on Ornithology, by P. L.
Hatch; on Entomology, by Allen Whitman; and on Geology of Rice
county, and L. B. Sperry. Also in the Regents’ Report for 1877. Out
of print.

THE SEVENTH ANNUAL REPORT, FOR 1878. 123 pp., 8vo.; with twenty-
one plates. By N. H. Winchell; with a field report, by C. W. Hall;
Chemical analyses. by S. F. Peckham; Ornithology, by P. ZL. Hatch;
a list of the plants of the north shore of lake Superior, by B. Juni;
and an Appendix by C. ZL. Herrick on the Microscopic Entomostraca
of Minnesota; twenty-one plates. Also in the Regents’ Report for
1878. Out of print.

THE EIGHTH ANNUAL REPORT, FOR 1879. 183 pp., 8vo.; one plate (Cas-
toroides). By N. H. Winchell; containing a statement of the Methods
of Miscroscopic Lithology, a discussion of the Cupriferous Series in
Minnesota, and descriptions of new species of Brachiopoda from the
Trenton and Hudson River formation; with reports on the Geology
of Centraland Western Minnesota, by Warren Upham; on the Lake

Superior region, by C. W. Hall; lists of birds and of plants from Lake
Superior, by Themas S. Roberts; Chemical Analyses, by S. F. Peckham;
Report by P. L. Hatch; and four Appendixes. Also in the Regents’
Report for 1879 and 1880. Out of print.

THE NINTH ANNUAL REPORT, FOR 1880. 392 pp., 8vo., three appendixes,
two wood cut illustrations and six plates. By N. H. Winchell. Con-
taining field descriptions of 442 crystalline rock samples, and notes on
their geological relations, from the northern part of the state, new
Brachiopoda, the water supply of the Rea River valley, and simple
tests of the qualities of water; with reports: on the upper Mississippi
region, by O. E. Gurrison; on the Hydrology of Minnesota, by C. &.
Terry; on the Glacial Drift ‘and its terminal moraines, by Warren
Upham; Chemical analysis, by J. A. Dodge; a list of the birds of Min-
nesota, by P. L. Hatch; and of the winter birds, by Thomas S. Roberts.
Also in the Regents’ Report for 1879 and 1880. Out of print.

THE TENTH ANNUAL REPORT, FOR 1881. 254 pp., 8vo., with ten wood
cut illustrations and fifteen plates. By NWN. H. Winchell. Containing
field descriptions of about four hundred rock samples, and notes on
their geological relations, continued from the last report; the Pots-
dam sandstone; typical thin sections of the rocks of the Cupiferous
series; and the deep well at the ‘tC’ Washburn mill, Minneapolis:
with geological notes, by J. H. Kloos; Chemical analyses, by J. A.
Dodge; and papers on the Crustacea of the fresh waters of Minnesota,
eleven plates, by C. L. Herrick. Also in the Regents’ Report for 1881

: and 1882. Out of print.

THE ELEVENTH ANNUAL REPORT, FOR 1882. 219 pp., 8vo., with three
wood cut illustrations and one plate. By WN. H. Winchell. Containing
a report on the Mineralogy of Minnesota, and a note on the age of
the rocks of the Mesabi and Vermilion iron districts; with papers on
thecrystalline rocks of Minnesota,by A. Strengand J. H. Kloos; on rock
outcrops in central Minnesota and on lake Agassiz, by Warren —
Upham; on the iron region of northern Minnesota, by Albert H. Chester;
Chemical analyses, by J. A. Dodge; and an Appendix containing
Minnesota laws relating to mines and mining, abstracted by C. L.
Herrick. Also in the Regents’ Report for 188! and 1882.

THE TWELFTH ANNUAL REPORT, FOR 1883. Summary report, containing ~
paleontological notes and a paper on the comparative strength of
Minnesota and New England granites, twenty-six pages, by N. H.
Winchell; final report on the Crustacea of Minnesota, included in the
orders of Cladocera and Copepoda, 192 pages and 30 plates, by C. L.
Herrick; and a catalogue of the Flora of Minnesota, 193 pages, with
one map showing the forest distribution, by Warren Upham. Also
in the Regents’ Report for 1883 and 1884. Out of print. :

THE THIRTEENTH ANNUAL REPORT. FOR 1884 196 pp. Geological |
reconnoissances, the Vermilion iron ores, the crystalline rocks of —
Minnesota and of the Northwest, the Humboldt salt-well in Kittson
county, records of various deep wells in the state, fossils from the
red quartzyte at Pipestone, reports on the New Orleans Exposition
and on the General Museum, by N. H. Winchell; Geology of Minne-
haha county, Dakota, by Warren Upham; Chemical report, by Prof.
J. A. Dodge; Minnesota geographical names derived from the

Dakota language, by Prof. Ax W. Williamson; Insects injurious to the
cabbage, by O. W. Oestlund; Geological notes in Blue Earth county,
by Prof. A. F. Bechdolt; and on a fossil elephant from Stockton, by
Prof. John Holzinger; papers on the Cretaceous fossils in the boulder
clays in the Northwest, by George M. Dawson and by Woodward and
Thomas; and notes on the Mammals of Big Stone lake and vicinity,
by C. L. Herrick. Out of print.

THE FOURTEENTH ANNUAL REPORT, FOR 1885. 354 pp.; two plates of
fossils and two wood cuts. By WN. H. Winchell. Containing summary
report, notes on some deep wells in Minnesota, descriptions of four
new species of fossils, a supposed natural alloy of copper and silver
from the north shore of lake Superior, and revision of the strati-
graphy of the Cambrian in Minnesota, with the following papers by
assistants, viz: List of the Aphidide of Minnesota with descriptions
of some new species, by O. W. Oestlund; Report on the Lower Silurian
Bryozoa, with preliminary descriptions of some new species, by H. O.
Ulrich; Conchological notes, by U. S. Grant; Bibliography of the Fo-
ramivifera, recent and fossil, by Anthony Woodward.

THE FIFTEENTH ANNUAL REPORT, FOR 1886. 493 pp., 8vo.; 120 diagram
illustrations and sketches in the text, and two colored maps; embrac-
ing reports on observations on the crystalline rocks in the northeast-
ern partof the state, by Alexander Winchell, N. A. Winchell and H. V.
Winchell; Chemical report by Prof. J. A. Dodge; additional railroad
elevations by N. H. Winchell; list of Minnesota geographical names
derived from the Chippewa language, by Rev. J. A. Gilfillan; and notes
on Illeni, describing three new species, by Aug. F. Foerste. Also as
supplement II of the Regents’ Report for 1887-1888. Out of print.

THE SIXTEENTH ANNUAL REPORT, FOR 1887. 504 pp., 8vo.; two plates
and 83 other illustrations. Contains reports on the originai Huronian
area, the Marquette iron region, on the Gogebic and Penokee iron-
bearing rocks, on the formations of northeastern Minnesota (includ-
ing the physical aspects. vegetation, quadrupeds and other verte-
brates), the geology of the region northwest from Vermilion lake to
Rainy lake and of the Little and Big Fork rivers: also notes on the
Molluscan fauna of Minnesota.

THE SEVENTEENTH ANNUAL REPORT, FOR 1888. 280 pp., 8vo.; ten text
illustrations. Contains: Report of N. H. Winchell, the crystalline
rocks of Minnesota, a general report of progress made in the study of
their field relations, with a bibliography of recent works on the crys-
talline rocks; report of H. V. Winchell, field observations in the iron
regions; report of U. S. Grant, geological observations in northeast-
ern Minnesota.

THE EIGHTEENTH ANNUAL REPORT, FOR 1889. 234 pp., 8vo. Report of
further field observations in the regions of the crystalline rocks of the
State and in the area of the original Huronian, by N. H. Winchell; and
a review of American opinion on the older rocks,by Alexander Winchell.

THE NINETEENTH ANNUAL REPORT, FOR 1890. 255 pp., 8vo.; with
illustrations. Translation of Boricky’s elements of anew Chemico-
microscopic method of analysis of rocks and minerals, and of Kloos’
Geognostic and Geographical observations in Minnesota in 1877, by
N. H. Winchell; Chemical report by Prof: Dodge; the woods of Minne-

sota, by H. B. Ayers; Museum and library additions; List of meteor-
ities in the museum: Petrography and geology of the Akeley lake
region, W. S. Bayley; New Lower Silurian Lamellibranchiata, EF.
O. Ulrich.

THE TWENTIETH ANNUAL REPORT, FOR 1891. 344 pp., 8vo.; 12

plates and 33 text illustrations. Summary statement; The crystal-
line rocks—some preliminary considerations as to their structures
and origin, by N. H. Winchell; Field notes in 1890, by N. H. Winchell;
Additional rock samples to illustrate notes, by N. H. Winchell; Field
observations on certain granitic areas in northeastern Minnesota, by
U. S. Grant; Catalogue of rock specimens, by U. S. Grant; The
Mesabi iron range, by H. V. Winchell; Sketch of the coastal
topography of the north side of lake Superior, with special
reference to the abandoned strands of lake Warren (the greatest
of the late Quaternary lakes of North America), by A. C. Law-
son; Diatomacez of Minnesota inter-Glacial peat, by B. W. Thomas,
(with list of species and some notes upon them, by H. L. Smith,
and directions for the preparation and moupting of Diatomaceex, by
C. Johnson and H. L. Smith); Oxide of manganese, by N. H. Winchell;
Museum additions; Additions to the Jibrary.

THE TWENTY-FIRST ANNUAL REPORT, FOR 1892. 171 pp., 8v0.; 2

plates and 21 text illustrations. Summary statement and compara-
tive nomenclature, with a table of the Pre-Siluran rocks of Minne-
sota aod their equivalents; The geology of Kekequabic lake in
northeastern Minnesota, with special reference to an augite soda-
granite, by U. S. Grant; Catalogue of rock specimens, by U. S. Grant;
Field observations in 1892, by N. H. Winchell; Some problems of the
Mesabi iron ore, by N. H. Winchell; Additional rock samples to illus-
trate report, by NV. H. Winchell; Additions to the library.

THE TWENTY-SECOND ANNUAL REPORT, FOR 1893 210 pp., 8vo.: 7 plates

and 3 text illustrations. Summary statement; Preliminary report of
field work during 1893 in northeastern Minnesota, chiefly relating to
the glacial drift, by Warren Upham; Preliminary report of field work
during 1893 in northeastern Minnesota, by U. S. Grant; List of rock
samples collected in 1893 by U. S. Grant; List of rock samples col-
lected in 1893, by A. D. Meeds; Preliminary report of a reconnoissance
in northwestern Minnesota during 1893. by J. EH. Todd; Notes on the
geology of Itasca county, Minnesota, by G. #. Culver; Preliminary
report of field work done in 18938, by J. #. Spurr; List of rock samples
collected in 1893, by J. H#. Spurr; Preliminary report of levelling
party, by C. P. Berkey; Preliminary report of field work during 1893
in northeastern Minnesota, by A. H. Elftman; List of rock samples
collected in 1893, by A. H. Elftman; Museum additions; Additions
to the library since the report for 1892; The exhibit of the survey at
the Columbian Exposition, by N. H. Winchell.

Il. FINAL REPORT.
(Distributed by the State Geologist.)

THE GEOLOGY OF MINNESOTA. VOL. 1 OF THE FINAL REPORT. 1872—

1882 xiv and 697 pp., quarto; illustrated by forty-three plates and
fifty-three figures. By N. H. Winchell; assisted by Warren Upham.
Containing an historical sketch of explorations and surveys in Minne-

ae ee ee ee

times:

RS ON igs Pee ae ee aE rt

Re Soe Sh os apieges

sota, the general physical features of the state, the building stones
and the Geology of Houston, Winona, Fillmore, Mower, Freeborn,
Pipestone, Rock and Rice counties, by N. H. Winchell; the Geology of
Olmsted, Dodge and Steele counties, by M. W. Harrington; and the
Geology of Waseca, Blue Earth, Faribault, Watonwan, Martin, Cot-
tonwood, Jackson, Murray, Nobles, Brown, Redwood, Yellow Medi-
cine, Lyon, Lincoln, Big Stone, Lac qui Parle and Le Sueur counties,
by Warren Upham. Distributed gratuitously to all public libraries
and county auditors’ offices in the state, to other state libraries and
state universities, and to leading geologists and scientific societies;
the remainder are held for sale at the cost of publication, $3.50 per
copy in cloth, or $5 in grained, half roan binding, upon application to
Prof. N. H. Winchell, Minneapolis.

THE GEOLOGY OF MINNESOTA. VOL. II OF THE FINAL REPORT. 1882—

1885, xxiv and 695 pp., quarto; illustrated by forty-two plates and
thirty-two figures. By N. H. Winchell, assisted by Warren Upham.
Containing chapters on the Geology of Wabasha, Goodhue, Dakota,
Hennepin, Ramsey and Washington counties, by N. H. Winchell; and
on Carver, Scott, Sibley, Nicollet, McLeod, Renville, Swift, Chip-
pewa, Kandiyohi, Meeker, Wright, Chisago, Isanti, Anoka, Benton,
Sherburne, Stearns, Douglas, Pope, Grant, Stevens, Wilkin, Traverse,
Otter Tail, Wadena, Todd, Crow Wing, Morrison, Mille Lacs, Kana-
bec, Pine, Becker and Clay counties, by Warren Upham. Distributed
according to law, in thesame manner as Vol. I above.

THE PALEONTOLOGY OF MINNESOTA. VoL. III OF THE FINAL RE-

10.

PORT. In press.

Ill. MISCELLANEOUS PUBLICATIONS.
(Distributed by the State Geologist.)

CIRCULAR No. 1. A copy of the law ordering the survey, and a note
asking the co-operation of citizens and others. 1872.

PEAT FOR DOMESTIC FUEL. 1874. Edited by S. F. Peckham.

REPORT OF THE SALT SPRING LANDS DUF THE STATE OF MINNE-
soTA. A history ofall official transactions relating to them, and a
statement of their amount and location. 1874. By N. H. Winchell.

A CATALOGUE OF THE PLANTS OF MINNESOTA. Prepared in 1865,
by 1. A. Lapham, contributed to the Geological and Natural His-
tory Survey of Minnesota, and published by the State Horticul-
tural Society in 1875.

CIRCULAR No.2. Relating to botany, and giving general directions
for collecting infomation on the flora of the state. 1876.

CIRCULAR NO.3. The establishment and organization of the Museum.
1877.

CIRCULAR No. 4. Relating to duplicates in the Museum and ex-
changes. 1878.

THE BUILDING STONES, CLAYS, LIMES, CEMENTS, ROOFING, FLAG-
GING AND PAVING STONES OF MINNESOTA. A special report by WN.
H. Winchell. 1880.

CIRCULAR No. 5. To Builders and Quarrymen. Relating to the col-
lection of two-inch cubes of building stones for physical tests of
strength, and for chemical examination, and samples of clay and
brick for the General Museum. 1880.

CIRCULAR No. 6. To ownersof mills and unim proved water-powers.
Relating to the hydrology, and water-powers of Minnesota. 1880.

[The miscellaneous publications are mostly out of print.]

IV. BULLETINS. wee

(Distributed by the State Geologist, except No. 9, which is distributed by the State

No.
No.

No.

THE METASPERM OF THE MINNESOTA VALLEY, a list of the higher

ile
2.

Neil

mon

-1

Botanist.)
History of Geological Surveys in Minnesota, 8vo., pp. 37. 1889, a
by N. H. Winchell. rr °

Preliminary description of the Peridotytes, Gabbros. Diabases!

and Andesytes of Minnesota. 8vo., pp 158: 12 colored plates. —
1887. By M. BE. Wadsworth.
Report of work done in Botany in the year 1886—1887. 8 vo., pp.
56. By J. C. Arthur. Out of print.
A Synopsis of the Aphidide of Minnesota. 8vo., pp. 100. 1887. By
O. W. Oestlund. :
Natural Gas in Minnesota. 8vo., pp. 39. 1889. By NW. H. Winchell. —
The Iron Ores of Minnesota. Their geology, discovery, develop-

ment, qualities and origin, and comparison with those of other —
iron districts, with a geological map, 26 figures and 44 plates. —

8vo., pp. 430. 1891. By N. H. Winchell and H. V. Winchell. i
The Mammals of Minnesota. A scientificand popular account of
their features and habits, with 23 figures and eight plates. 8vo.,

pp. 300. 1892. By C. L. Herrick. !

The Anorthosytes of the Minnesota coast of Lake Superior, by A.
C. Lawson. The laccolitic sills of the northwest coast of Lake
Superior, by A.C. Lawson. Prefatory note on the Norian of
the Northwest. by V. H. Winchell. 8vo., pp. xxxiv, 48: 7 plates
and 8 text illustrations. 1893.

PartI. Prefatory note. On the occurrence of Sphagnum atolls
in central Minnesota, by Conway MacMillan. Some extension
of plant ranges, by HE. P. Sheldon. On the nomenclature of
some North American species of Astragalus, by E. P. Sheldon.
List of fresh water Algz collected in Minnesota during 1893, by
Josephine E. Tilden. On the poisonous influence of Cypripedium
spectabile and Cypripedium pubescens, by D. T. MacDougal 8vo.,
pp., 1-38, three plates. Jan. 16, 1894.

PartIl. Nitrogen assimilation by Isopyrum biternatum, by D. T.
MacDougal. On the morphology of hepatic elaters, with special
reference to branching eiaters of Conocephalus conicus. by J.
E. Tilden. Revised descriptions of the Minnesota Astragali, by
E. P. Sheldon. Synonymy of the North American species of Jun-
codes, With further nomenclatural notes on Astragalus, by E. P.
Sheldon. Further extensions of plant ranges, by #. P. Sheldon.
Determinations of some Minnesota lichens by W. D. Frost.
8vo., pp. 39-85, three plates. March 21, 1894.

Part. I1I. A revision of the Mucoracee, with special reference
to species reported from North America, by Roscoe Pound. Re-
vision of the Minnesota grasses of the tribe Hordeew by Francis

Ramaley. A perliminary list of the North American species of —

Astragalus, by E. P. Sheldon. 8vo., pp., 86-176. June 8, 1894. —
ParT1IV. On a new registering balance, by A. P. Anderson.

‘J

On a new electrical auxanometer and continuous recorder, by __

free nitrogen by plants, by D. 7. MacDougal. 8vo.pp. 177-222, ~

four plates. Sept. 27, 1894.

No. 10. The Iron-Bearing Rocks of the Mesabi Rangein Minnesota. With

22 figures and 12 plates. 8vo.,p. viii, 268. 1894. by J. Edward

Spurr. octet

V. BOTANICAL SERIES. ae

(Distributed by the State Botanist.)

dé,

seed-producing plants indigenous to the drainage basin ofthe —

Minnesota river, by Conway MacMillan. 8vo., pp. 826. 1892.

VI. ZOOLOGICAL SERIES. an
(Distributed by the State Zoologist.)

y
a

First REPORT OF THE STATE ZOOLOGIST, accompanied with notes on the —

birds of Minnesota, by P. L. Hatch. 8vo., pp. 387. 1892.

, _

= =.
»%
oe,

Geological and Natural History of
QE Minnesota.
127 Report
Al15
Ve22d
Physical &
Applied Sci.
Serials

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