Sh > a ares ee ee ee ees ee
cs SB. Soc sO Re eo a goa eowatios. HK fans [ ewe] aaa] s = «faecal
Sertiaia. Siro) > on Ree een ola OR dc dha Wheel Ge ee X |...) 50 -)e eee
NORETIONE BN. 6 Es RSE ce eek a CO saat ee we luant X Jann oan
Stantonoceras pseudocostatum
Johnson. .|...]..-|.-.1 2? -}<..1 X fe. }. 2 ole ee
Syncyclonema rigida H. & M.......)...|... ya ee eee ee -
SURCYCIONEMAIE SBIs Oe Recreate Red eee eon x} Ke
TOs SCURRI Mi ie A. ee AS Ce on MP ee
“yo CPUSBec tetas. ffs Sa eiseeeee Meier 4 os Bea Gas fre = =| + 0's] sim =e ie
a SSB. Geb Pe Elec ate ie ene hk SE AER en gh cn Mente Mc wa eee <~ 10 Seas
Thetis. circul@nis,M..& > Hic esc nccs~ Pas al oes RR ne « <.ils Je
Trigonarca (Breviarca) exigua
“ce
SMe ak Seieiiae eet ee ls ee JCSReeS o|. » =| sn y mare oes a a
“¢ trinervis Kn : sPactaasie tee eee eee . Te Be
CRETE | Tol Roy Roms CNG < Shu SMa pee iy) 0! Sauk te Saad eee
ANGUAGE SP 0:3 ccece 0/0 kia ree eee oes eels a Se eee eee
Syncycionemea rigida I. & Me coos ook csi aoe oe eee ee oe
ce SDiis e's eas s bia cuseeate beac A EE bee ete eee eee
x
be oblongus: Meek 2.0). cast ets oon ee eee
M OGAOUG SP Fe ye iots fase Watatcs eRe ew tole eee Rie ge nae ae eee
Cardi: speciosa: Moi Hee nie Bia akc aide ais ee eee
Pinna Tahest, WHI tiie oneness cals orecin bee Seas he eee ee eee
Trigonarca (Breviarca) epigua M: & Hi... i ee sec cece ene
Lucinga occitentanhs: CMorton) occ. 2ece s cece caweee sn cena ee
Thetis cireutaris Me & Boe Pees bo ae ee ee ee
PYTATUSUCMSDE Soak Hea lek 0 Cae REE Ee wae Ge ee eee eee
PCARRD ic he Sova es bth Kin Rib nial sos epahauelee Ss ape Se Geen ae ee
RE GCUIOT SD e ip aicea SO Ce wae eters So ee ee ee ee
LAOpistha Undale Ma Rec. 5. .0asie xt ek sk ae me se oleic ele ere
EMT IST 6 in x Se Ses es las SS ee ee ak nla CE Re eee
ae tee Rk
Te PR eR DS
x xX XK XK X
2S. Pa OPER. oh
ACTED: Sao stye bik stave les eee ne es Sieea oe ede ene Sl cen Oebecere
ELTON CEGED stn San Belcan a la sion castes ee Aa Roane aoe eee ee
BOCuUIIeS OVUGTES SAV Oe es cee ews eh Aes Oe eee hn ee 2 ee
ss COULPFESSUS: Says o2 Oe aletare’e <,Macd ele che ahers were levi siarkietens
xxxXxxXxxXxXxxXxXXXX
sé macercaiare.. Mo>& Hoss e.ks io ets oe ee eee
Eigh) “SCHIES oy nee ee a oh aw ako he When oe oc tae ate ciel ee
There is above the Lewis shale a series of rocks not less than 1,000
feet thick, somewhat shaly in the lower part, where a thin bed of coal
occurs, but consisting principally of massive sandstone more or less con-
glomeratic throughout. Apparently some of the older geologists referred
this whole series to the Laramie. Others referred some of it to the Lara-
mie and some to the Tertiary. Schrader (100) described the lower or
coal-bearing portion as “Laramie,” and proved, by tracing the beds, that
it is identical with the “Laramie” of the Durango region. The following
DESCRIPTIVE DETAILS: MONERO AND DULCE 617
fossil plants were found by the present writer a few feet above the coal
both north and south of the railroad near Dulce:
Fossil Plants collected from the “Laramie” near Dulce, New Mexico
(United States Geological Survey locality number 6042)
(Those marked (*) occur also in the “Laramie” near Durango, Colorado)
*Brachyphyllum macrocarpum Newb.
*Sequoia reichenbachi (Gein.) Heer
Cunninghamites sp.?
*Geimitzia formosa Heer.
Palm (same as species at Point of Rocks)
Ficus planicostata ? Lesq. (Same as species at Point of Rocks)
*Ficus n. sp. (8-nerved)
*Ficus lanceolata Heer
Zizyphus n. sp.
~The flora is essentially the same as that described from the “Laramie”
of the Durango section, and confirms the statement that the beds are of
the same age. It also strengthens Doctor Knowlton’s opinion, previously
quoted, that the beds may be older than Laramie, inasmuch as two of the
species are found at Point of Rocks, Wyoming, in a formation regarded
as older than Laramie, and others are found in the Mesaverde at the
localities farther south, described in this paper. In commenting on these
plants, Knowlton says: “Their age is essentially Montana and not Lara-
mie. If uninfluenced by their apparent stratigraphic position, I should
incline to place them in the Mesaverde, but since they are above Lewis
they obviously can not be Mesaverde, though they can be—and in my
opinion are—still Montana.”
The writer found no invertebrates in the “Laramie” near Dulce, but
J. H. Gardner collected some from this formation near Pagosa Junction,
about 15 miles northwest of Dulce. They are as follows:
Fossils collected in southeast One-quarter, Section 19, Township 34 North,
Range 4 West, near Pagosa Junction, Colorado, 5 feet above
Laramie (?) Coal Number 1
Ostrea subtrigonalis EB. & SS. Corbicula cytheriformis M. & H.
Anomia sp. cf. A. micronema Meek Corbula undifera Meek
The rocks above the Lewis shale in the Dulce area, referable to the
Cretaceous, are only about 225 feet thick, including the basal sandstone,
which is 60 feet thick. A section of them and of the rocks underlying
them was measured in the steep canyon wall about a mile northwest of
Dulce. At this locality a conglomerate that varies greatly in thickness
618 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
and character within short distances rests unconformably on the coal-
bearing rocks. For about 75 feet above this basal conglomerate the rock
is variable in lithologic character and consists of friable, granular sand-
stone and shale, irregularly intermingled, and in it are many lenses and
irregular masses of conglomerate. The whole mass is dark colored and
gives the impression of being the erosional product of a mass of dark-
colored igneous rock. The suggestion is offered that this formation may
represent the Animas formation of the Durango region, although its
stratigraphic position would tend to make it somewhat older than the
Animas.
Section of Rocks measured about one Mile Northwest of Dulce, New Mexico
Feet
Sandstone, conglomeratic, Drown: . ..<.205.6 52.4 eek sk ae 2 80+
Sandstone, slightly shaly, with greenish tint at base; massive, yellow
ADOVE] |S ab oS Rhare ares GE eas ale wiv S 21d apa Se eas Wee ee 44
Shale -and ‘sandstone, yellow vc We ssc wes ba eete te 2 oe eee 121
Sandstone, shaly; greenish. voc 00... Ss awe cee ces cece eee eee 6
Conglomerate with pebbles, principally of chert, up to one-half inch
MN GIAMELCT ois es haw 0 es che ee eta oe Siete ereie eee ete ereioin ic Rlete tee 12°
Sandstone, shaky, (gray... O06 0 Sake see ee Le ee ee at
Conglomerate with chert pebbles up to three-quarters inch in diameter 28
Shale; Sandy, ¥ellow o.%jo.55 wile eres eetereteye Seale ele a 8
Sandstone; WHC. eck arelcrare wl cise ook ec ae aete sree eee ee 3
Shale, sandy, yellow . 2. 0.0% ss'Gai ees. 5 6 8 we ws o's Re oats 6 er anaes Oe 10
Conglomerate with chert pebbles up to three-quarters inch in diameter 38
Shale, sandy, Fellow oo73 az oe Pek, wie FS meen who S eww fetatin he wee eae 18
Sandstone, massive, coarse-grained, yellow..............ccccecnccce ‘ 66
Shaie, ‘sandy, dark-colored: «is cclhc s dae nists Sas Rise weed i oR yAl
Sandstone; friable; dark-colored: i020)... 0.22%. wa.s% as seu ae 46
Sandstone, coarse-grained, conglomeratic, with pebbles mostly of chert
up to ar inéh or more in’diameter......52.....4 Je. e. » ss ee 6
(Unconformity by erosion. )
Shale, sandy, carbonaceous; contains fossil leaves (U. S. G. S. locality
INO. GO42) ee Os Scan 2S nck 2 Oe Des rege oe ACA 83
Coal, ‘coke; and. intruded igneous rock... o/c. sts 2s 2s bee Se 8
Sandstone, coarse-erained, light-colored... 02... .2.:.. 0626 e.se toe eee 66
Shale, ‘SAREY os sotieels oo Se hte ee Fe eae oe 8
Sandstone, massive, light-colored. ... 2. 5.0 vases «= is cu oe wien ee 60
Shale (Lewis), fossiliferous (U. S. G. S. locality Nos. 7200 and 7201). 300+
The writer found no fossils in rocks above the unconformity, but other
geologists seem to have been more fortunate. J. H. Gardner, who is
familiar with this region, has, at the writer’s request, furnished the fol-
lowing information in a letter dated December 26, 1911:
DESCRIPTIVE DETAILS: CABEZON 619
“T have carried a reconnaissance survey around the north side of the San
Juan Basin and have done the détails of the Ignacio folio which lies to the
west but on the rim of the same basin. There is no doubt in my mind, based
on reconnaissance mapping and lithological similarity, that the beds to which
you refer (those above the unconformity) are Animas. . . . The heavy
conglomerate beds at the base of the Animas are in the form of a lentil which
thins out away from the Animas Valley. The beds above this consist of tan-
colored and greenish shale alternating with coarse-grained, tan-colored sand-
stone containing grains of igneous origin. . . . The beds which are intruded
with sills along the canyon and cross-cut by dikes (the upper 461 feet of the
foregoing section) are of the same nature and apparently connect with the
upper beds of the Animas. They are older than the Puerco and Torrejon,
and contain remains of Triceratops.”
CABEZON
The writer made few observations between Dulce and Cabezon, a dis-
tance of about 90 miles. Doctor Gardner (116) correlated the rock for-
mations exposed near Cabezon with those of the Durango region and gave
them the same names, namely, Mancos, Mesaverde, Lewis, and “Lara-
mie.” ‘The correlation is based on the work of tracing the outcrops of
these formations around the San Juan Basin from their type locality in
southwest Colorado. ‘They are described as more or less continuously
exposed on the west and south sides of the basin, but for a short distance
west of Nacimienta Mountains they are covered by overlapping Tertiary
rocks. However, in spite of the great length of outcrop around the basin
to the west and the area of obscured outcrops on the east side, Doctor
Gardner seems to have felt confident that the formations near Cabezon
are to be correlated directly with those of the Durango section. He col-
lected fossils from both the Lewis shale and the Mesaverde formations.
They are among the United States Geological Survey collections and
have been identified by T. W. Stanton. Two collections were obtained
from the Lewis as follows:
Invertebrates collected by J. H. Gardner from about 100 Feet below the Top of
the Lewis Shale about 6 Miles Southeast of Raton Spring, New Mezico
(United States Geological Survey locality number 4455)
Ostrea sp. Liopistha undata M. & H.
Cardium speciosum M. & H. Lunatia sp.
Legumen sp. Melania? sp.
Invertebrates collected from the Lewis Shale by J. H. Gardner two and one-
half Miles Southeast of Cuba, New Mexico
(United States Geological Survey locality number 4452)
Inoceramus barabini Morton Placenticeras intercalare M. & H.
Baculites compressus Say
XLIV—BULL. Grou, Soc. AM., Vou. 23, 1911
620 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
His Mesaverde fossils, collected near Cuba, are as follows:
Invertebrates collected'near the Base of the Mesaverde Formation, three-
quarters of a Mile North of Copper City, New Mexico
(United States Geological Survey locality number 4453)
Nucula sp. Volutoderma sp.
Cucullea sp. Acteon sp.
Arca sp. Baculites anceps var. obtusus Meek
Cardium sp. Placenticeras intercalare M. & H.
Cyprimeria? sp. Placenticeras sp.
Liopistha undata M. & H. Heliococeras sp.
Mactra sp. Scaphites sp. related to S. larveformis
Gyrodes sp. M. & H.
Pyrifusus? sp.
While in the field the present writer assumed that the Mesaverde age
of the coal measures near Cabezon was established, and bis purpose in
visiting this locality was to collect fossils from the Mesaverde for the
purpose of correlating with it the coal-bearing rocks which in the fields |
farther east contain similar fossils. A large number of petrified logs and ~
stumps of trees were found in the lower part of the Mesaverde north of
Cabezon, and leaf impressions occur in the same beds, but most of these
were too poorly preserved for identification. However, beautifully pre-
served leaves were found in a thin layer of fine-grained sandstone about
400 feet above the lowest bed of coal. The locality is about 5 miles
northwest of Cabezon, in a steep bluff half a mile north of a small arti-
ficial lake. The species collected are as follows:
Fossil Plants collected from the Mesaverde Formation, North 43 Degrees West
from Cabezon Butte
(United States Geological Survey locality number 6038)
Ficus speciosissima Ward
Ficus n. sp. (8-nerved)
Dryopteris Dp. sp. (Same species found in lower group of coal
beds at Canyon City, Colorado)
Dyospyros sp.
Ficus 0. sp.
Myrica sp.
Eucalyptus sp.
Dombeyopsis? sp.
Two or three undescribed dicotyledons
Fragments of palm leaves were found 50 to 100 feet above the bed
yielding these plants, but no fragment was found with the parts necessary
for the identification of species. Still higher in the formation, at the
\
DESCRIPTIVE DETAILS: CABEZON 621
east end of Chacra Mesa, several conifers of the species Abietites dubius
Lesq. were found.
Two small collections of shells were made from the Mancos shale near
Cabezon. One was obtained from the sandy layers at the top of the for-
mation in the transitional zone between the Mancos and the basal sand-
stone of the Mesaverde. They were found at the point where the wagon
road leading northwestward from Cabezon crosses the top of the Mancos
shale. They are as follows:
Fossils from the Top of the Mancos Shale, Northwest of Cabezon
(United States Geological Survey locality number 7194)
Ostrea elegantula Newberry ? Mactra sp., related to M. formosa M.
Anomia sp. & H.
Pinna sp. Corbula sp.
Cardium sp. Gyrodes sp.
Cyprimeria sp. Act@won sp.
Tellina sp. Placenticeras sancarlosense Hyatt
Liopistha undata M. & H.?
The second collection was obtained from the low hill back of the town:
of Cabezon at a horizon several hundred feet below the top of the Mancos
shale. The rocks containing them are somewhat sandy, and this fact may
serve to explain the resemblance of the fauna to that yielded by the sand-
stones of the Mesaverde. The fossils are as follows:
Fossil Shells collected at Cabezon, New Mexico
(United States Geological Survey locality number 7195)
Exzogyra@ sp. Gyrodes sp.
Anomia sp. Volutomorpha sp.
Avicula linguiformis BE. & §S. Volutoderma ? sp.
Inoceramus barabini Morton? Liopeplum sp.
Mytilus sp. Pyrifusus ? sp.
Cucullea sp. Placenticeras sancarlosense Hyatt?
Crassatellites ? sp. Stantonoceras pseudocostatum Johnson?
Cyprimeria sp. Lamna sp. (shark’s teeth)
From a study of fossils collected from the Mancos, in the vicinity of
Cabezon, Shimer and Blodgett (109, page 58) arrived at the conclusion
that the shale was of Benton age. They found many Benton species asso-
ciated with a few which they regarded as belonging to the Pierre fauna.
However, the exact horizons of their collections are not known to the
present writer, and it is possible that they may be somewhat lower than
the horizons at which the fossils named above were found. In the light
of the more recent investigations, Doctor Stanton is of the opinion that
622 w.tT. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
these fossils belong to the fauna occurring in the coal measures in the
Rio Puerco field, which in turn are referred by him to the lower part of
the Montana.
Shimer and Blodgett describe the Mancos shale from several localities
between Cabezon and the Rio Puerco field. They report a characteristic
Benton fauna from low in the shale corresponding to the Concretion
(Septaria) zone of Herrick and Johnson, and a separate fauna from
higher in this shale supposed to correspond in general with the Caphalo-
pod zone of Herrick and Johnson. ‘The upper zone of these writers con-
tains a large number of Benton species, together with a few which they
regard as characteristic of the Pierre (see 109). Their work serves to
connect the formations observed near Cabezon with those of the Rio
Puerco field, for although the Mesaverde is not continuous between the
two fields the Mancos is continuous and the overlying Mesaverde occurs
in Prieta Mesa and probably also at Cabezon Butte, so that there are only
three short breaks in its continuity between the large area occupied by
this formation in the San Juan Basin and the smaller area in Rio Puerco
field.
RIO PUERCO FIELD
Aside from brief references in the accounts of early explorations to the
occurrence of coal, the first geologic information of the Rio Puerco coal
field was given by Herrick and Johnson (77). The various zones de-
scribed by them and the fossils contained in each zone are named in the
notes of the annotated list of publications (77) in the latter part of this
paper. These zones were found convenient for use by the present writer
and are here used in a quotational way.
The Cretaceous rocks of this field dip toward the east, the degree of
dip varying greatly from place to place, and disappear under a cover of
Tertiary and Quaternary rocks in the Rio Grande Valley. A section
showing the main features of the Cretaceous rocks below the Mesaverde
was measured near San Francisco. The line along which the measure-
ments were made extends across the gently dipping rocks from the Da-
kota (?) outcrop northwest of San Francisco to Punta de la Mesa farther
to the south. ‘The fossils collected from the several horizons are named
in the section:
Section of Rocks measured in the Rio Puerco Coal Field near San Francisco,
New Mevzico
Feet
Sandstone, massive, yellow (Punta de la Mesa sandstone or base of
MeS&VETUE) |. s'nis vos koe 6 ws nem e alek's & Guin nadine aie oe ee ee eee 77
Shale, sandy-8t top. co io ss os ke wee we cee he esl cetera eae 240+
Limestone, shaly, containing Ostrea lugubris Conrad and Coilopoceras
colleti Hyatt (U. S. G. S. locality No. 533) 5) eee 10+
DESCRIPTIVE DETAILS: RIO PUERCO FIELD 623
Feet
ee a a OS ene ere Ruarals oine are\c wue'e Weamiewe Sens oe kod 50
Shale with limestone concretions (Cephalopod zone) containing Pinna
petrina White?; Pecten sp.; Trigonarca sp.; Isocardia sp.; Veniella ?
sp.; Cardium sp.; Turritella sp.; Volutoderma sp.; undetermined
gastropods; Metoicoceras sp. related to M. swallovi (Shumard) ;
meroscoceras sp. (U.S. G. S. locality No: 3520) 2.0... cee ccc ween’ 10+
Shale. In the lower part were found Ostrea sp.; Avicula gastrodes
Meek; Pinna petrina White; Veniella sp.; Pholadomya sp.; Twrri-
tella sp. related to 7’. whitei Stanton; Metoicoceras sp. (U. S. G. S.
locality No. 7191). The fossils were collected at some distance from
the line of measurement of the section and may possibly belong to
RITES (ANI S oC Scie dea ew ea nl be we die ws wd Reldie aleve owe eon 600+
Sandstone, shaly, with impure limestone in lenses and concretions.
(This sandstone and the limestone concretions above and below it
seem to constitute the Concretion (Septaria) zone of Herrick and
Johnson.) It contains Ostrea sp.; Hxogyra columbella Meek;
Anomia sp.; Avicula gastrodes Meek; Cardium sp.; Legumen sp. ;
Pecten sp.; Pinna petrina White; Isocardia sp.; Liopistha (Psilo-
mya) sp.; Anchura sp.; Prionotropis sp.; Acanthoceras ? sp. (U. S.
ate INOS. (192 ANG Sib) «5 cane cece cence e eee eucmecannes 50
Shale alternating with layers of yellow sandstone.................. 78
Shale, carbonaceous, dark-colored; has general aspect of the shale
associated with the coal beds of the Mesaverde in this field...... 2
Sandstone, coarse-grained above, shaly below; weathers to irregular,
rounded masses; contains Halymenites similar to H. major Lesq.,
worm borings, and a variety of indefinite markings.............. 25
Shale, dark-colored (Gastropod zone), containing Ostrea sp.; Exogyra
columbella Meek; Camptonectes symmetrica Herrick and Johnson;
Plicatula sp.; Gervilliopsis ? sp.; Pinna petrina White; Pinna sp.;
Liopistha (Psilomya) sp.; Arca sp.; Trigonarca sp.; Cardium sp.;
Lucina sp.; Turritella sp.; Anchura fusiformis White non Meek;
Anchura sp.; Cinulia ? sp.; Serpula sp. (U. 8. G. S. locality Nos.
RE SITE SUPER Po eo Sn ig cea 0 oda we Walco ue sla nb wees eue 35
Sandstone, soft, friable; contains small pebbles, principally of quartz
TERR ne See laa ate oi ele. Sina asa 2 Sieck ow alk Stee e's an viele ale 5
Me RYU a's onc s wie ant aoe cu ea awe ats Caldne éwadin eet wae aa eee s 8
(Abrupt change in lithology.)
Sandstone, coarse-grained, gray to pink; varies greatly from place to
place in thickness, composition, and color. This sandstone has the
stratigraphic position of the Dakota, but its color and variable char-
re NEP COIVe. OF MGETIOON. clic sh adn sc ca cece seas nvanes wewes 100
Sandstone and shale, variegated (Morrison).
1,290
Two collections of fossils were made east of the Rio Puerco about 3
miles north of San Francisco. The first is from a zone of limestone con-
cretions that seems to occupy a horizon about 50 feet above the top of the
624 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Tres Hermanos sandstone. The following species were collected at this
locality :
Fossil Shells collected East of the Rio Puerco, about 3 Miles North of San
Francisco, New Mezico
(United States Geological Survey locality number 7204)
Ostrea sp. Turritella sp.
Pinna petrina White Prionotropis sp.
Cardium sp. Metoicoceras sp.
Lunatia sp. Coilopoceras colleti Hyatt
The second collection is from an exposure about half a mile east of the
first and estimated to be stratigraphically higher by about 100 feet. The
strata here dip very slightly to the east and the rocks are covered with
soil in most places. The shells collected at the higher horizon are as
follows:
Shells collected East of the Rio Puerco, about 3 Miles North of San Francisco,
New Mexico
(United States Geological Survey locality number 7193)
Ostrea lugubris Conrad Baculites gracilis Shumard?
Anomia sp. Prionocyelus wyomingensis Meek
Inoceramus fragilis H. & M. Scaphites warreni M. & H.
Anchura sp. Ptychodus sp. (fish teeth)
Anisomyon ? sp.
These fossils seem to indicate horizons several hundred feet above the
base of the Mancos, namely, near the Caphalopod zone, whereas their
apparent position as observed in the field is near the base of the Mancos
about 500 feet below the Caphalopod zone. It is possible that the rocks
have been faulted, so that the position of this zone in the section is de-
ceptive, but no indication of faults with displacement of more than 25
feet was noted near these localities. |
More detailed investigation of the Mancos from Rio Puerco westward
is necessary before its subdivisions and their relations to each other and
to neighboring formations are properly understood. The rocks dip at
low angles and broad grassy valleys occur at the outcrops of the shale.
The rocks are faulted and warped in some parts of this field, and it is
difficult to find a place where there is no liability of error in measuring
the shale in these broad valleys. Furthermore, the fauna is not so well
known that the vertical range of all the species can be confidently given.
A section measured by Darton (114, page 60) near Laguna, at the
southwestern extremity of the area shown on the accompanying map, is
DESCRIPTIVE DETAILS: RIO PUERCO FIELD 625
given. The fossils seen indicate a position near the base of the Mancos
about the horizon of the Tres Hermanos sandstone, and yet they occur
above a body of shale much thicker than any reported elsewhere below
this sandstone.
Section of Part of Cretaceous Rocks 2 Miles Northeast of Laguna, New Mezico
Measured by N. H. Darton
Feet
SOE Satan's: «a's Se iided i, denial worn e a Cite Meee ki le iw aie, a) @oese ai Stata ett We Shetae 2%
0 su His ad GEC ieee o eid sie aim.d bite, Wh he, abel 25
oe eave calc saie ald also « diaks nies cnare GER Ste ONE'S bn'au Win’ aim misread, a0) 4 Alea an 60
ssanastone, buff, massive, moderately soft.........-.ccccccscesceccess 40
Shale with sandstone layers, very fossiliferous; contains Hxogyra colum-
bella Meek ; Gryphea'sp.; probably a variety of G. newberryi; Avicula
gastrodes Meek?; Cardium sp.; Panopea sp.; Turritella sp.; Rostel-
eM IsrOUeT INGE Sp.; ANG: FUSUS SP «swe 'w wis 6 sisperse ons ak on Fe mean wawsine fs
nernacnive:. Nard, LONG, DUG yo. 5 sae s.s.ie o.6 0100.00 oieh wind’ 'ns 50 0 /q > 40
Shale, dark gray to gray-green, sandy layers fossiliferous; contains
Ezxogyra columbella Meek; Pecten sp.; Pinna petrina White; Inoce-
ramus ? sp.; Leda sp.; Cardium sp.; Lucina? sp.; Isocardia n. sp.;
Cyprimeria? sp.; Corbula sp.; Liopistha (Psilomya) concentrica Stan-
ton; Turritella whitei Stanton; Tritonium Kanabense Stanton; Actwon
Poems Sp.; Turrilites? sp., or Heterocerads Sp......cccaacascsees 60
EE PTET ST CET BRESEDV 5 oe oa ec le a ave wip aie ais 6, a0, she ac a 'e.eie bin eRe tee ee 5
Sandstone, white, massive, part coarse................ SSE ES, ear aes 80
Shale, greenish gray, sandy above......... pA AS Ci 9, panel ears Ai 235
rat E BUEL, TWASSIVG oo cia. caw ace ce cm ese eadnedeees mae Ss ad what 2 40
Ee oa ins 1G /s tan eee u thé aie aia'<'u sa wjeraye whace’« ¢ eve CoN uheas «6 30
eae ei OL, CFeLICCOUS) . oe ice ce ca vac ewes cee vevecsetess
oh) ee a Pe etd date Hebe a trek o we dine: 4 sina wa's Fie ata tiie: « 490
No place was found where a complete detailed section of the Mesaverde
formation of the Rio Puerco field could be measured. The beds are well
exposed in only a few places, and where they are exposed some of them
are warped to such an extent that it is difficult to trace individual beds
for any considerable distance, and others are faulted so that certain beds
are duplicated; also, some of the upper part of the formation seems to
have been removed by erosion previous to the deposition of the overlying
Tertiary rocks, inasmuch as the lowest bed observed in the Tertiary is a
conglomerate. A generalized section was measured east of the Rio
Puerco, about 3 miles north of San Ygnacio, where many fossils were
collected. A section of the upper part of the coal-bearing rocks was
measured in detail about a mile farther north by L. C. Chapman, who
was assisting the writer in doing the field work. This has been incor-
porated in the general section below. Where the section was measured,
626 w.T,. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
faulting has occurred in a way that renders the relation of the Mesaverde
to the Tertiary open to question; but near the northern end of the Rio
Puerco field an exposure was found of rocks undisturbed by faulting
where the basal conglomerate of the Tertiary with pebbles of quartzite
up to 6 inches in diameter rests on the Mesaverde.
Section of Mesaverde Rocks measured near San Ygnacio, New Mexico
Feet Inches
Sandstone, locally conglomeratic, and shale (Tertiary) poorly
consolidated, vari-colored, with reds predominating below and
milder shades above (many hundreds of feet).................
Probable unconformity...... PDN ne mci Sg BBs 5
Shale with thin beds of coal; absent in some places.............. 0-10
Sandstone, massive, yellow, calcareous, and shaly in some places;
contains Ostrea sp., Anomia sp., Inoceramus sp. (thick-shelled) ;
Cucullea sp.; Cardium sp. (large form) ; Cardiwm sp. (slender
form) ; Tellina sp.; Cyprimeria sp.; Liopistha undata M. & H.?;
Corbula sp.; Mactra sp., related to M. formosa M. & H.; Mactra
sp. (large form) ; Dentalium sp.; Gyrodes sp.; Physa ? sp.; Volu-
tomorpha novimexicana Herrick & Johnson; Pyropsis sp.; Ac-
twon ?sp.; Scapnites sp., related to S. nodosus Owen; Placen-
ticeras sancarlosense Hyatt?; Placenticeras planum Hyatt? (U.
S:.-G.7S. locality ING TISO ee sean ek cuca erage cre ete ae a ee 300+
Shale, sandy, containing Brachyphyllum ? sp.; Ficus n. sp. (3-
nerved type) ; Salix ? sp.; Ficus ? sp. (large leaf) (U. S. G. S.
locality No; GOSE)s oe 8 SoS Sa Sos Sete Oe eee 9
Shale; carbonaceous £007 S ie ic reise tae ee Bie en Skee Oe ee AE ‘
Coal tea. o Oia Bh TESS Bee lee ee Ge eon ween beats at ee af 1
Shale; carbonaceouse soc he eae en le oe da win era OI Ce ee 7
Sandstomes sete £924 See See re inien I ss eee Oe ee ee 8 -
Shale, CarbOnaceOus oe Vine oe we es ee ks Sikes Oe ee ee eee 2 6
COA so can ts Ses ae nol eee AUS eo Riclo Me oa bs Bun oua'e wel « Ooe eRe ie fe ¥ ¢
Shale; “CarbOnacéoussek ores oe hee: oe oo obs eee ores ee oe 3 6
SanGSt@nes tars ta hele see eka See sw EES els od sie ate tye aie ate See ris
COa] m ihe Rice Races sie tis iat bac wares Sie dele'k eos Ree ee oh a
Shale, -CaRDOMACCOUS ss sae ahs Cae « od 2% Asie SRM eb ele ee ee 7 ie
GOAT is. spaneie eine toll ate ale aalls ie WPS 69s 40 Swe Sie elle sae Ne a 6
Shale, CAFDOMACEOUS As os sche s coke ware & alee ecwie’ 4 ote elm che GER OR eee 10 a
Coal ereakts et ele ec oc we en bc be ree eee oe he eee * 2
Shale, -Carbonaceousei ns cms OWok bes bala tly ic 6. J ee 2 6
SANGSEODE 125 chee yes Wie NU otel ew Hie po ole eaca Sib e me, peels See STE eee if
Shale 25 veiling win site ee i eee ae © Ace bow» oe Oa Re 6 *
COST, Seis Setete tere a ridin bcs. vo epee ws bic 6 wle:a ied alta denen ie 5
Shale, CarboMBceous). 5.5 dyn hs oc 2 i's a wane wae bisieiae sc ah eo eee 3 6
Coal Ree eles are Bie: oe ose Se was Caleta cove Cate ne 2
Shale, Sa@Mgyinc é «2 were evs Meta we Wide bia le’o eualecdeg Rigtetatae APRESS 2 6
COB aes a hag eben ew k GR lech in Jes wo ole nel ead el te Ree 1
M
my
ah
2
mM
9
B
Qu
|
fan)
DESCRIPTIVE DETAILS: RIO PUERCO FIELD
627
Feet Inches
EN Ee Ce oak tale tk < cos & oR a SURI Kiewit WoW blew ha a vo walew ee 2
aN GOO. 4 RE pela, wats; Bio's Mee vee sere 1
EP PERPEENAS oie tah v's Weniee d's d's s
EE RETE TT COONES 5 5. boc + sin f SRI eM Sete We 68 a's oS wd la che case 2
is my DOE Rg eee aera Ce eo bs
Pensa i. Ota. Stems ke RRR Se Cea eC eared eee ewe 3
nett OAT SE-P TANCE . o.oo sys Sataelesla eee eee Vs OUR be sae e ee 2
EE ESEISCETINEES 9. 6 05 WS ac bau whe ee ea ne Bk hk oR ee eB ns 3
Me ater el tars shn{a 6 ue @ winys nin wp aheceberanetae, bon wl etw's xi ain"s, 26% a « 1
aE TARISESNIEE TIES © 5 oc. a0 65's c" sini's nono. c CNET Ble eee wee sls weld Bei ae a5
ee eee Fee ete aiid et ETS others gta ek hid 6 RKO Rie ES Be
EERIE TEPER Nat 2165. hac vcs <'oin.k Gels b's eas wis Wate aie bias 'atee vg dee 4
a ee a ee ee 1
REE ERO ACCOUS . 02 cco a sw ais oie <.5 2 ae wa biew neve oa eae ee we 8
NTN Fone ye ain l'on pct nlm Som ees socks ‘ea mien. n Bale be) Wie wa kh
IIE SOMEART hes 2a he gcc) diac 'c wrt Gidea A © ale ob ad Oleialae ew & 6 2
Pe FOR NESE-PTAINGG, STAY 6.5 cost een cee ct tee enc ceseeeeese 3
See curponaceous, Chocolate-colored.......... ccc ccc ccc ccvens 5
a Nee a ee ee ¢
Shale, carbonaceous, chocolate-colored.......... ccc cece cccccces Zz
Sandstone, coarse-grained, MaSSive, ZTay.............ee eee eeeees 30
_ Shale, with layers and lenses of yellow sandstone and earthy
limestone containing Halymenites major Lesq.; Ostrea congesta
Conrad; Jnoceramus sp.; Lithophagus ? sp.; Lamna sp. (U. S.
EOIN 1 MO in tea ne a Rook wha on ew aw Slane e Gee hl ood dle we 400+
Sandstone, coarse-grained, yellow to gray; contains the following
fossil leaves: Quercus sp. serrate, new; Ficus n. sp. (3-nerved
type) ; Ficus sp.; Dryophyllum falcatwm Ward (Point of Rocks
species) ; Dalbergia n. sp. (same as Hagan No. 6030); Salia
stantoni ? Kn.; Viburnum ? problematicus Kn. (U. 8. G. S. lo-
MME SSS OST) RCA Silt aoa yk oy 2 ayo aa cto ays oe 25+
Shale, containing one bed of coal 6 feet thick and several thin
Sandstone with layers of shale and lenses of impure limestone,
meiterous, but no collections made: ....0..6..0.ceesccuscees 172
Sandstone, massive, gray, with lenses of impure yellow limestone
near the top, containing Ostrea sp.; Inoceramus sp. (very thick-
shelled form) ; Cucullea sp.; Cardiwm sp.; Tellina sp.; Liopistha
undata M. & H.?; Mactra sp. related to M. formosa M. and H.;
Mactra sp., large form; Volutomorpha novimexicana Herrick &
Johnson ; Baculites sp.; Placenticeras planum Hyatt; Lamna sp.
ne ere ape, NE TOS PROUD oracle oe chen bb didin ies Pee VC va eles 110
Shale, carbonaceous, chocolate-colored...........ccccccccecvecce 27
Sandstone, yellow, and shale, in alternating layers............... 235
6
1
6
628 Ww. tT. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
= SECTION AT HOLMES MINE
7 400"
’
INDEX MAP
=
Q
g TAIN. REE.
&
9
C SS SS
WE eave ater ge
8 we .
N 50" Vi oh ort wang
x eels 3; RTOCCO MINE. X=
== : Eee Biren ee ee S
eres Teak Ld XY
55 :
RSE WS
ies
15”
2"
15!
== 5
: , Mi
30 {
eae Poke
po Zz
a 1S
: F
LEGEND
Mesaverde forrnation
San Antonio/
WN Mancos shele
SS
Coal mine
[2 |Site and dip
ULI TPS 2
)
Z
_—S
LISS
7
~~
Lo
Scale
1
2 MILES
Figure 4.—Map of Tijeras Coal Field, New Mexico
ca a
"ss
DESCRIPTIVE DETAILS: TIJERAS COAL FIELD 629
Feet Inches
Site, yellow to chocolate-colored. .... 6... cc cc ccc recccccccccces 57
PMc A TPIEITECOOTIO ¢ av. le dig lee olka the aid kvae. ack amnn dana
RE are A ON See tind. Ga he Ae Rl ubtnlS ace snlg CAS eieh eo
SEER eed ae ocr alin re W aged me wie do gE miele Caw e andes Bia a
PAAR TET EVOL ORAS SS ais bo srasideeianad oc wae cree wesc
Shale (Mancos), sandy in the upper part, with lenses
and concretions of sandstone. .......ccccccccccccce
13
5,895 +
The Mancos shale is well exposed west of the outcrop of the Mesaverde
and does not differ in any essential manner from the Mancos of the
As at Hagan, the lower part consists mainly of dark-
colored shale and the upper part of sandy shale which weathers to a yel-
Hagan section.
642 w.T,. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
lowish brown color and contains fossiliferous concretions of impure lime-
stone. No coal or carbonaceous shale was found below the sandstone that
is here regarded as the base of the Mesaverde. The sandy shale is re-
garded as the transitional zone at the top of the Mancos, although it is
quite possible it may be the equivalent in time of the lower part of the
Mesaverde of other localities.
At the base of the measured section occurs a massive sandstone that
appears to be at the same horizon as that at the base of the Mesaverde at
Hagan. Five coal beds exposed in the mine entries, now abandoned, and
several prospect openings were observed above this massive sandstone.
The coals apparently hold the same position as those previously described
from the Sloan and Hagan mines. Fossil plants were found at several
horizons closely associated with the coal beds and several were collected —
principally from the sandstone and shale overlying the main coal bed.
They are named as lot number 6028 in the accompanying section.
There is a series of shales and sandstones above the coal-bearing rocks
containing ironstone concretions. These rocks may be the time equiva-
lent of the rocks constituting the highest shaly member of the Mesaverde
at Hagan. On them, as at Hagan, a conglomerate rests unconformably.
It is the basal conglomerate of the colored rocks which are correlated in
a. general. way with the Galisteo sandstone of the Cerrillos field. They
contain great numbers of petrified logs, some of them very large. The
state of preservation of most of them is poor and no specific determina-
tions have been made. No identifiable fossils have been found in these
colored rocks and their geologic age is not definitely known.
The coarse conglomerate which overlies the colored beds is composed
principally of igneous material derived from the Ortiz Mountains. It
consists of angular blocks of igneous rock varying in diameter from a
few inches to several feet. The material is irregularly bedded and the
beds dip eastward by about the same degree (30 degrees) as the underly-
ing rocks. The thickness obtained by correcting for dip the distances
measured across the strike in the upper part of the gulch, locally known
as Devils Canyon, is about 3,000 feet, but this may be in excess of the
actual thickness, for the bedding is too irregular to admit of accurate
determinations of thickness. It is certain, however, that this conglomerate
is many hundreds of feet in thickness. It is the same as the youngest
conglomerate of the Hagan section that was described as lying uncon-
formably on the: Galisteo (?), Mesaverde, and Mancos formations.
CERRILLOS FIELD
The Cerrillos coal field is better known than those just described,
mainly because of the productive mines which have been operated here
DESCRIPTIVE DETAILS: CERRILLOS FIELD 643
for many years. The coal-bearing rocks occupy a syncline between the
Ortiz Mountains and Galisteo Creek and extend from the town of Galis-
teo westward for a distance of about 14 miles. The syncline is unsym-
metrical and the rocks are warped and faulted in many places, but in
general they dip from all directions toward the center of the syncline.
The general geology of this field has been described by D. W. Johnson
(83), and no space will be devoted to it in this paper farther than is
necessary for an understanding of the age and structural relations of the
Cretaceous and younger formations. The coal-bearing rocks are referred
to the Mesaverde and are correlated with those of the Hagan, Tijeras,
Rio Puerco, and Cabezon coal fields, as indicated in figure 2.
The principal coal beds of the upper part of the Mesaverde formation
have been opened at Madrid and their thickness, character, and strati-
» graphic position are well known from mining operations. Coal has been
mined from three beds, the lowest of which, known as the Cook and White
coal bed, averages 3 feet in thickness. One hundred feet stratigraphic-
ally above this is the Peacock coal bed, averaging 1 foot 8 inches in
thickness, and 22 feet higher is the White Ash coal, which normally con-
tains coking bituminous coal, averaging 5 feet 6 inches in thickness. Near
Madrid this White Ash coal has been changed to anthracite by the intru-
sion above the bed of a sheet of igneous rock 400 to 500 feet thick. The
anthracite coal averages 3 feet in thickness. From data obtained in min-
ing and kindly furnished to the writer by Mr. G. A. Kaseman, the follow-
ing section of the coal-bearing rocks at Madrid has been constructed.
This section probably furnishes the best standard with which to compare
others measured in the Cerrillos coal field, although fossils are so scarce
as to be of little assistance in correlating other sections with it.
Section of Rocks exposed at Madrid, New Mezico
Feet Inches
Intrusive igneous rock
shale, containing fossil plants; Geinitzia sp.........ec cece nee eee 5 baum 2
ARTY DEG. -... 500 ok dee cee sf uls ww Wee ie ale wes 5 6
MITTEE SENIE S os, ow oa ie vied an eats eos knew hawk wens 22 i
EE TE CEOSEGN LIENS «or ots 50's oe a hy es. rn ww aa wa CY we Oo 1 8
DIRT EENI TES 30 -oc's 5 ci ie cas mapeeae la Eh GES S Sac w w Ala Wiwdieee ak WANs 8
CRS fe koe a wwe Sa ce eile Cee iS ea ema eae oa he kr 20
TIN ee hla ug ka Sa 2 nent WERE Be savas @ 0/0ld wie RE Stee 6 oa 20
Oy ie aS ons 554+ ale ¢s UR MIWAG We'w deh ox ae SAK ha ake 20
SIEEY COL NOMI OE. COME... pods os wad we avin s 6 cd ous SRlwhe Ge we 2
Eas Data Wee's eects wie POR elaa Sica a vaca ce nee kbc. 6
CRO Aa ore Leela a. Op art as" aha ie ota Oe id Go Gms 6 Gia e Rha Oban 20
RS a ad wt ee ee ache y dev Wore: Ga Vine Lh a boheme 3
mec MINS AMEE CMV TIMES SIEGE. 0 oC oc dae vkac odieemeeceseeuase 3
644 w.tT. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Madrid Waldo Mesa Rogers
Ft. In.
A:
: E
2| 5
3|?
a) 3
a| 3
ai
7
§ felor 4
E
)
E
Fy 85
§ LEGEND
oe
|2002
i Igneous rocks
7180 7164
Fossil locality TGS £ =
Vertical scale =
eager 0 100 200Feet 5
9 miles == iy pul. <2 ae =
F1IGuRB 5.—Geologic Sections and Drill Records in the Cerrillos Coal Field, New Mezico
DESCRIPTIVE DETAILS: CERRILLOS FIELD 645
Feet Inches
MITE NS aeg Ee ETI no en «oc he PRON OS bow ep Re Coen ewnn ae & 5
CEOEEEE Sohne SA ae, outer eie se’ np Birk vs Siw hed eeee een midhe oe 16
NE tot. aa Ca ete san a WRN OEE Gh keeles ete we ele iw one 8 bx
OS gy et emery Se OE Se ee ee _ 11
ER Ure. , gO wk ucg aco MRR S CME NS eae uikic e's @ bie Sitio hie 9
ER nN au a.nd al iat OME aN a Ves Ow hede daw ee xn 8
IO RTO 8. cc cals C446 LER OR CR CeE veetbuusweteusns 16
191 9
Few fossils were found in the coal-bearing rocks at Madrid, although
careful search was made for them. The shale beds overlying the coal in
the mines near Madrid were searched, but at only one locality were fossil
plants found in them. This is about a mile south of Madrid in the roof
of a prospect opening in the White Ash coal bed, where conifers, identi-
fied as probably belonging to the genus Geinitzia, were found in shale
above the coal. Where the Cook and White bed crosses Coal Gulch north
of Madrid this coal bed is overlain by a massive sandstone in which are
pinkish brown concretions of sandstone. Im one of these concretions
were found impressions of shells similar in appearance to some of the
shells of marine origin that occur so abundantly in the sandstones at the
- base of the Mesaverde. The writer found no other shells above the coal
beds near Madrid, but J. J. Stevenson (53, page 155) reports the occur-
rence of Inoceramus and Ostrea in the coal-bearing rocks.
The rocks at Madrid dip east about 15 degrees, and the mine entries
have been driven down this dip under an intrusive sheet of igneous rock
which forms the crest of a hill east of the town. Above this sheet and
in a gulch about half a mile east of Madrid coal-bearing rocks are ex-
posed near the mouth of an abandoned mine. The following section was
measured by D. W. Johnson (83, page 107) at this locality and the sec-
tion was later confirmed by the present writer. To the fossil plants
reported by Doctor Johnson have been added those collected by the
_ writer.
Section of Rocks measured at an abandoned Coal Mine one-half Mile East of
Madrid, New Mexico
Feet
Penna (CE ATE CONCERIO€ 6. ica. wefan div tdi und W Svinte aiec aecelnte cane ihe
ROL de yeaa Gite oe Pomc cis ou awa wnat ese dweiens vee & 1
IR OMIEU Saat c've a dinta dade a Delee Ce Oc yay © Ei ic aRie wuterviee be Whee ee wece 8
rE oaw i, CHPEE LS Lg ats sok Me ah eee wes end hd Wale wu munieule delete eke 3
MERE OR OURS Ee WS Jccre i cis = Gate Min ches! a ale Gale Wann enield ced be t.e wane 10
Sandstone, indurated, containing Ficus rhamnoides Kn.; Ficus uncata
Lesq.; Ficus speciosissima ? Ward; Ficus sp. type F. planicostata
Lesq.; Palmocarpon commune ? Lesq.; Geonomites sp.; Quercus ? sp.;
ae? Ge CO. S. C.. 8. locality No: GOIS). 2c. cic ride eecweesva 9
646 w.T.LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Feet
Shale, CarhbonaceGGss cigs o6rc cg cas ca cca eck weap ee cue oes ieee 10
SanGstone oy fos sce dw dh we Wee eons acre 0-20 6 ae 4,51 4 & ate Relea pe eke tee ne 6
Intruded: Java: SHEGE 6.5 Se cd oan ce eye 6 es oS care are ene eee 10
SHAG idee ies 65 hale Be CER Sree bs Oc ee ee we ban Sine prainie te alee Ono 4
Gosek cea ees eh une wale e's 0 C Cable Ree Sane ere 2
SBTC e548 & ois) bod iw a ase is aie cw Dio poo 0.0 ke cea ge a 3
66-+-
The rocks of this section lie stratigraphically below the Galisteo sand-
stone and above the intrusive sheet of igneous rock that overlies the
highest or White Ash coal bed at Madrid. The thickness of this intruded
rock is shown in the accompanying records of drill-holes. A diamond
drill prospect was made in the gulch a few hundred feet northeast of the
old mine just mentioned and about 4,500 feet east of the principal open-
ing at the outcrop of the White Ash coal bed. The drill penetrated some-
thing like 75 feet of rock that seems to belong to the Galisteo sandstone
before it reached the coal-bearing rocks of the Mesaverde, and then en-
countered beds that seem to be equivalent to those of the section just
given. After passing through the igneous rock, a group of coal beds was
encountered that doubtless is the same as those opened at Madrid. The
record is platted to scale in the third column of figure 5, on page 644.
A second drill-hole was put down 6,800 feet east of the outcrop of the
White Ash coal bed. The drill reached a depth of 1,602 feet and pene-
trated not only the beds represented in the first record, but those of strati-
graphic horizons considerably lower. The Galisteo sandstone occupies
the surface in this region, but there is nothing in the record to indicate
its thickness at this locality except the red or variegated color, which,
however, may be caused by the metamorphic action of the intrusive igne-
ous rock. Since no coal is known to occur in the Galisteo sandstone, it
seems safe to draw the line of separation between this formation and the
Mesaverde above the highest coal bed, as has been done in figure 5.
This record shows the occurrence of three groups of coals. The highest
group obviously corresponds with that represented by the beds under-
neath the sheet of intrusive rock in the first record and to those of the
Madrid section. The two lower groups probably correspond in strati-
graphic position to those described later near Omera farther east and to
the lower coals near Rogers west of Madrid. The record is platted to
scale in the second column of figure 5.
The dip of the rocks, which is 15 degrees east at Madrid, if unchanged
would soon carry a given bed to a considerable depth. However, the
dip no doubt lessens eastward toward the center of the basin, and it is
DESCRIPTIVE DETAILS: CERRILLOS FIELD 647
probable that the 1,602-foot hole extends entirely through the Mesaverde
formation. The surface in the center is occupied by the Galisteo sand-
stone and younger rocks, but the underlying Mesaverde reappears from
beneath them with opposite dip at the eastern extremity of the basin and
was observed near the town of Galisteo, although no details of it were
obtained there. However, at the southeastern extremity of the basin one
of the Mesaverde coals has been developed at Omera mine. A section of
the rocks exposed near this mine was measured. The dip is low, and the
thicknesses given in the following section were obtained by pacing across
the outcrop and correcting for dip. Hence the:section is approximately
correct, but it is presented only for the purpose of showing the relation
of the Mesaverde formation to the underlying matt shale and to the
overlying Galisteo sandstone.
Section of Rocks measured at Omera Mine, about 18 Miles Southeast of
Cerrillos, New Mexico ,
Feet Inches
Conglomerates base of Galisteo sandstone.
(Unconformity. )
onl (Omers, MME)... 63 sas caene mee Meee 2+
rT COTTER. 2 cies ain ccdie de nie’ Nine oe am «OK 0 6
Shale, with layers of sandstone and cone-in-cone
structure limestone (not continuously exposed).. 75 2%
(0 0, SER TT Duh OES ae eS en eee, > eae pee era ee Ba TODS oc
Mesaverde Shale, Carbonaceous in some piaces, with lenses
and concretions of sandstone, and cone-in-cone
structure limestone. Fossil plants at the base... 85
COA Fees 2: Be ce eh Sha ah Re Ws AX ale Scracae ipisie a eats 0 4
EB rer circ She ee eh eee dew eck he dae 5
Sandstone, massive, yellow; contains fossil shells... 200+ ..
Shale (Mancos) with a sandy transitional zone at
the top. Concretions of fossiliferous limestone
occur 100 to 150 feet from the top; containing
Exogyra ponderosa Roemer ?; Anomia sp.; Ino-
ceramus sagensis Owen ?; Thacotndies sp. ; Cucul-
lea sp.; Cyprimeria sp.; Volutoderma ? sp.;
Nautilus sp.; Baculites sp.; Mortoniceras sp. re-
lated to M. delawarense (Morton) ; Placenticeras
sancarlosense Hyatt; Placenticeras sp.—very
large specimens, apparently distinct from either
of the foregoing (U. S. G. S. locality No. 7180).
A few hundred feet lower in this shale the follow-
. ing fossils occur: Crassatellites shumardi Meek ?;
Mactra sp.; Gyrodes sp.; Volutoderma? sp.;
Acteon ? sp. (U. S. G. §. locality No. 7181).....
648 Ww. T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
A comparison of this section with the 1,602-foot drill record seems to
show that the lowest bed of coal, which is only 4 inches thick where the
section was measured, but which is somewhat thicker in other places,
corresponds in stratigraphic position with the lowest coal beds represented
in that record ; that the 100-foot sandstone of this section finds its coun-
terpart in the 169-foot sandstone of the drill record, and that the coal
developed in the Omera mine corresponds in position with the middle
group of coal beds of the drill record and with the lowest developed coal
of the Rogers section (see figure 5). If this correlation is correct it is
evident that a large part of the Mesaverde formation as represented in
other parts of the Cerrillos coal field is not present at Omera, and that
the unconformity above the Omera coal represents an erosion interval of
long duration.
As indicated in the foregoing section, the conglomerate of the Galisteo
sandstone rests in some places directly on a coal bed. This bed varies
considerably in thickness within short distances. In some places where
shale intervenes between the coal and the overlying conglomeratic sand-
stone the coal bed is 4 to 5 feet thick. In other places where the con-
glomeratic sandstone rests on it the coal is thinner and in some localities
is entirely replaced by the sandstone. This was found to be the case in
the mine workings. J. H. Gardner states in his unpublished notes of the
Omera mine that 560 feet down an old slope the coal suddenly disappears
against a face of sandstone showing no evidence of faulting. He found
that this disappearance was due to total erosion of the coal bed previous
to the deposition of the sandstone. He also states that at one locality
near Omera mine he found two coal beds separated by 9 feet of sandstone,
the lower one 3 feet thick and the upper one 4 feet 6 inches thick. At
one of the prospect entries, a few rods from the place where the Omera
mine section given above was measured, the present writer observed two
coal beds as follows:
Section of Rocks measured near Omera Mine
Feet Inches
Conglomerate with pebbles of several kinds of rock, including an-
Sulat ErarimentS ‘OF ‘COAL. s. o:dn ot was cos s cake els oe ee
CRUE Sita Sale swe cnld,e '» wie win sm cle Vin etuln'e'e cae ee Re oe ee ee 0 2
STG SIME cn wae io wisn 'c.n'u 0 ce oes 1a 0 aie he's) ei oor ee 2 6
fo A A ee ee Ea ORE eA 4 2
SAIC cis Skee eG ne dee ha'e ous ois sb ache >» an a pigeon ee eae
DESCRIPTIVE DETAILS: CERRILLOS FIELD 649
The conglomerate shown at the top of this section constitutes the base
of the Galisteo sandstone. In it were found pebbles and boulders up to
6 inches or more in diameter, consisting of quartz, chert, sandstone,
limestone, petrified wood, coal, etcetera. This formation is exposed con-
tinuously from Omera northward to Galisteo Creek and westward to
Madrid.
Below the Mesaverde the Mancos shale occurs in characteristic devel-
opment. Great numbers of fossils, especially cephalopods, occur in con-
eretions of limestone near the top of the formation. The species collected
here are named in the accompanying section. The thickness of the
Mancos was estimated to be about the same as that given for it in the
Rogers section, but no attempt was made to measure it. It dips gently
toward the west and occupies the broad valley on either side of the Santa
Fe Central Railroad. At the eastern side of this valley, about 3 miles
east of the town of Galisteo, a few Benton fossils were collected. They
are Ostrea sp., Inoceramus fragilis H. & M., Prionotropis sp., and unde-
termined casts of pelecypods and gastropods (United States Geological
Survey locality number 7170).
About 2 miles south of the locality where these fossils were collected
the Tres Hermanos sandstone was recognized, and between this sandstone
and the Dakota the shale which contains the Gastropod zone at the locali-
ties described farther west. Below the Mancos shale is a hard conglom-
eratic sandstone which, on the basis of lithologic character and strati-
graphic position, is referred to the Dakota, and under it are variegated
sandstone and shale that probably are Morrison.
The rock formations above the Morrison in this eastern limb of the
syncline correspond closely with those in the western limb, but below the
Morrison there seems to be a difference. Hast of Omera a massive, cliff-
making sandstone, about 100 feet thick, pink to red in color, occurs below
the Morrison and lies unconformably on the deep red and purple sand-
stone and shale of the typical red bed formation of this region. This
sandstone has the appearance of the Exeter sandstone (81, page 45) of
eastern New Mexico and holds the same stratigraphic position. It was
not recognized in the western limb of the syncline in the Cerrillos field,
nor farther southwest in the Hagan and Tijeras fields, although it may
be represented west of the Rio Puerco by a red cliff-making sandstone
which occurs below the Morrison. Below this sandstone east of Omera
occur red rocks similar to the Manzano red beds that underlie the Morri-
son west of the Cerrillos field.
The line of outcrop of the coal beds extends from Omera in a north-
westerly direction and seems to pass around the northern base of the
650 w. TT. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Ortiz Mountains to the coal in the vicinity of Madrid, but in the inter-
vening space the coal is covered with debris from the mountains. North
of Omera the coal beds were displaced by the intrusion of the igneous
rock of Cerro Pelon, which rests on the basal sandstone of the Mesaverde
at its southern end and on Mancos shale farther north. This shale and
basal sandstone were observed underlying the Galisteo sandstone north
of Cerro Pelon in the vicinity of the town of Galisteo, but no indication
was found that any coal occurs there. It seems probable that the erosion
which preceded the formation of the Galisteo sandstone removed all
rocks that may have existed above the basal sandstone of the Mesaverde
in the vicinity of Galisteo. Little was seen of the Mesaverde or of the
older rocks between Galisteo and Cerrillos. They are covered for the
most part by younger rocks, but near Cerrillos the Mancos and Mesaverde
reappear in vertical position upturned by the intrusion of the igneous
rocks of the mountains north of this town.
West of Cerrillos the rocks dip steeply to the south and Galisteo Creek
flows in a gorge cut along the strike partly in the Mancos shale and
partly in the basal sandstone of the Mesaverde formation. About one
and one-half miles west of Cerrillos the rocks are well exposed south of
the stream, and a section was examined carefully for the purpose of locat-
ing the coal beds which have been developed at Rogers, a coal-mining
camp west of Madrid, now abandoned. At the horizon where the main
coal beds should occur coal was found, but the beds are thin, possibly
due to crushing at the time the rocks were upturned. Otherwise the sec-
tion at this locality does not differ materially from the Rogers section.
which follows, except that the base of the Galisteo sandstone is more
coarsely conglomeratic than it is at Rogers. It consists here of hard
quartzose sandstone containing pebbles principally of quartz and chert
up to an inch or more in diameter.
Fossil plants were found at this locality at a horizon about 325 feet
above the top of the basal sandstone of the Mesaverde. They occur in
shale in a railroad cut on the branch line from Waldo to Madrid. They
are as follows:
Fossil Leaves collected in a Railroad Cut one and one-half Miles West of
Cerrillos
(United States Geological Survey locality number 6021)
Brachyphyllum sp. Ficus lanceolata Heer
Celastrus n. sp. Ficus n. sp. (8-nerved)
Ficus speciosissima Ward
i |
DESCRIPTIVE DETAILS: CERRILLOS FIELD 651
South and west of the locality just described on Galisteo Creek the
rock formations are well exposed and were traced to Rogers, an aban-
doned coal camp situated on the western limb of the syncline. ‘The rocks
strike nearly north and south and dip 9 degrees east. A section was
measured by tapeline from the old Rogers mine westward across the
strike of the upturned rocks to a point at the base of the Cretaceous about
a mile south of Galisteo Creek. This section may be combined with the
Galisteo Canyon section of the Manzano group published by the writer
several years ago (110 B, page 18).
Section of Rocks measured near the old Rogers Mine, two Miles southwest of
Cerrillos, New Mexico
Feet Inches
Conglomerate (Recent).
2 ESS | oe er gee een © em eae 25)
Per aERA RES! READ O ig 8 ait a nd caine aera bh Elkan 8
SES TT a ee Eo 16
UTERINE: SIREN VES 6 tothe cw, a Sate Sis Rie Ge wine Res pa ac « 12
Serer. TIT COOTEN. i cs Sain « cae Foc mn keie oe eule 15
: eneEehNe: SEMAN VE ( SPAY. Sa. ok en o'e $4 wb wine wie Qs em os 10
Galisteo 1 Shale and sandstone in alternating layers......... 68
Sandstone, massive, coarse-grained, friable, loose-
textured to quartzose; locally conglomeratic;
variable in thickness and character; contains
fossil plants; Abietites dubius (?) Lesq.; Geono-
mites sp.; Dryopteris ? Sp........0.ccecccees wites © DES
. (Unconformity by erosion.)
Coal, thickness irregular, due to erosion;
resis TOI IAOPS oa dn es mc ee kw es at
Sandstone, shale, and thin beds of coal in alternat-
ing layers; contains fossil leaves, conifers and
Nelumbo intermedia 7 KM... 5... ccc ceca cccceves 65
froel. ( HOPES GEM Re ) aces ais eye die wae week oe +
Shale and sandstone; the shale carbonaceous in
some places with thin seams of coal............. 105
Sandstone in massive layers separated by thin beds
of shale; forms the crest of a ridge............. 105
Sieaiverde Sandstone and shale in Perrine layers; contains
concretions of brown sandstone................. 146
PRN tO Mee a hid das vy ere 4 ee wee SA Se 1
EN ORE UG so RS 5
OS gO pS ae ee Ay A ei a a a 2+
ON ie AR ed Mek Os Deccan hoe co Bratere 4% dw die ede id 31
Cs RM eae inti eh 4's hm A ite wend sain ew we i+
Shale with yellowish limestone concretions, con-
taining Ostrea sp. related to O. soleniscus Meek.. 15
OB MS ert and a ee ey Poe eee ee 0 6
PUTER EE PO re ie Cn oe h aig eek bo nines’ awe hve 5
NR et PE Auta ck wal Gh hw lnie a Wes aible’s bla > aids 0 6
_ XLVI-—BvLL, GzoL, Soc, AM., Vou, 23, 1911
652 Ww.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Feet Inches
Sandstone, principally massive, light gray, friable
in some places with brown fiinty concretions.
Thickness varies from place to place, but the
lower 50 feet or more forms a prominent cliff—the
Mesaverde basal sandstone of the Mesaverde—aund contains:
Halymenites major Lesq.; Mactra sp. related to
M. alta M. and H.; and several gastropods and
other shells similar to those found below the
basal sandstone... ... 02050. Loe eeee ns ee eee 300+
( Shale with thin layers of gray sandstone; consti-
| tutes the transition zone from the shale below to
the base of the Mesaverde; contains Ostrea ele-
gantula Newberry?; Anomia sp.; Inoceramus sp.
related to J. proximus Tuomey; Jnoceramus sp.
related to J. barabini Morton; Cucullea sp.;
Cardium sp.; Cyprimeria sp.; Legwmen? sp.;
Corbula sp.; Mactra? sp.; Anatina sp.; Denta-
lium sp.; Turritella galisteoensis Johnson; Vo-
lutomorpha sp.; Volutoderma? sp.; Nautilus
dekayt Morton ?; Scaphites sp. related to S. hip-
pocrepis De ‘ay Baculites sp.; Placenticeras
sancarlosense Hyatt; Placenticeras planum Hyatt
(U. S. G. S. localities Nos. 7164 and 7165)....... 150+
Shale, dark-colored, with fossiliferous concretions
Mancos of limestone near the top and near the bottom. . 2,100
Sandstone (Tres Hermanos), hard, quartzose in
thin, irregular layers; weathers yellowish brown;
contains shells, numerous worm borings, and in-
definite markings of various kinds; also Haly-
menites major Lesq.; Pinna petrina White ?;
Pecten sp.; Gyrodes sp.; Turritella sp. (U. S.
G. S. locality No.°T1G8) ....s. 265 2 eee ee 20
Shale, dark-colored, with dark brown concretions
of impure limestone (Gastropod zone) and a
stratum of “crinkly” sandstone one foot thick
\ pear the middle... .. 20. 2.
years ago” (that is, about 1835).
The coal-bearing rocks are referred to the Cretaceous,
BIBLIOGRAPHY AND NOTES 667
No. Date.
42. 1875. Lorw, Oscar: Geological and mineralogical report on portions of
Colorado and New Mexico.
Geographical explorations and surveys west of the 100th
meridian, by Wheeler, annual report. Annual Report of the
Chief of Engineers for 1875, part II, Appendix LL, pp. 101T-
1036. Washington, 1875.
(Appendix LL is published in separate form, pp. 1-196. 1875.)
(Pp. 1023-1026) Cretaceous coal measures west of Nacimiento
Mountains are described; also (p. 1027) those of the Rio Puerco
field.
(P. 1028) The anthracite at Placer Mountain was examined;
also the coal in Tijeras Canyon and other New Mexico localities.
43. 1876. Meek, F. B.: Descriptions of the Cretaceous fossils collected on
the San Juan exploring expedition under Macomb.
Report of expedition from Santa Fe, New Mexico, to the
junction of the Grand and Green rivers of the Great Colorado
of the West, in 1859, under Macomb; geological report by New-
berry, pp. 119-133, plates, 4°. Washington, 1876. ;
The fossils described in this report were collected by New-
berry in 1859 from the Cretaceous rocks of western New Mexico
and Colorado.
(Pp. 121-122) Meek agrees with Newberry in correlating the
“Lower Cretaceous” of the latter with the Dakota of the Upper
Missouri Cretaceous section, the “Middle Cretaceous” with the
Benton and Niobrara formations, and the “Upper Cretaceous”
except the highest beds, which were regarded as probably Ter-
tiary, with Pierre and Fox Hills.
44, 1876. NEWBERRY, JOHN S.: Geological report. Report of expedition from
Santa Fe, New Mexico, to the junction of the Grand and Green
rivers of the Great Colorado of the West, in 1859, under the
command of Capt. J. N. Macomb, pp. 9-118, map. plates, 4°.
Washington, 1876.
Abstract, Am. Jour. Sci., 3d series, vol. 13, pp. 220-221 (4% p.).
1876.
The Cretaceous is subdivided into three groups; the lowest or
“Tower Cretaceous” includes the Dakota of other writers; the
“Middle Cretaceous” is made equivalent to Benton and Nio-
brara, and the “Upper Cretaceous” to the Pierre and Fox Hills
(including beds at the top that later proved to be Tertiary).
(P. 38) “Triassic rocks containing . . . Silicified trunks of
coniferous trees” are reported east of Cerrillos. (The silicified
trees east of Cerrillos described by later writers are in the
Galisteo sandstone. )
(Pp. 38 and 51) Near the mouth of Galisteo Creek, and also
east of the town of Galisteo, fossil leaves said to be of Creta-
ceous age were found in yellow sandstone below the marine
Cretaceous shale. (The description seems to indicate that these
may be in rocks older than the Dakota of the present paper.)
XLVII—BULL. GroL. Soc. AM., Vou, 28, 1911
668 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
45.
46.
47.
187
Date.
1877
The coal beds at the base of Placer Mountain (the Mesaverde
near Madrid) are referred to “Middle Cretaceous,’ and the
bituminous coal is described as changed to anthracite by igneous
intrusion.
(Pp. 67-71) In northern New Mexico (north of Jemez Moun-
tains) the three subdivisions of the Cretaceous were recognized
and traced westward through southwestern Colorado. The
rocks near Sierra del Navajo (near the Colorado-New Mexico
line) are described as ‘‘Middle’ and “Upper Cretaceous.” (The
Mesaverde, Lewis, and “Laramie” formations of later writers.)
(P. 117) The “Brown sandstones and beds of lignite” near
Nacimiento are referred to “Middle Cretaceous.” (These are
clearly the Mesaverde rocks of later writers.)
. Corr, E. D.: Report on the extinct Vertebrata obtained in New
Mexico by parties of the expedition of 1874.
United States geographical surveys west of the 100th merid-
ian, Wheeler in charge, Reports, vol. 4, paleontology, 370 pages,
plates 22-83, 4°. Washington, 1877
Abstract, Am. Jour. Sci., 3d Laer 15, p. 56 (14 p.). 1878.
(Pp. 1-13) The Cretaceous west of Nacimiento and Gallinas
Mountains is described and a cross-section given showing coal
in “Cretaceous No. 3” (probably the Mesaverde), succeeded
after a covered interval by Puerco.
(Pp. 13-25) The relations of the Eocene to the Ceafadenan
are discussed at some length.
7. HAYDEN, F. V.: United States geological and geographical surveys
of the Territories; geological and geographieal atlas of Colo-
rado and portions of adjacent territory, by F. V. Hayden, folio
22, double folio atlas sheets, 35 by 2234 inches. Washington,
1877 (second edition 1881).
Detailed geologic sheets, by Endlich, W. H. Holmes, Peale,
Marvine, and C. A. White.
The Cretaceous and younger formations mapped in north-
western New Mexico are Dakota, Colorado (including Benton
and Niobrara), Fox Hills (including Fox Hills proper and
Pierre), Laramie, and Wasatch.
The marine shale (apparently both Mancos and Lewis), in
northern New Mexico west of the Rocky Mountains, is mapped
as Colorado shale. The coal-bearing rocks (apparently includ-
ing both Mesaverde and “Laramie” and probably including also
some of the Tertiary) are mapped as Fox Hills. The Wasatch
is mapped as resting on the Fox Hills at the eastern margin of
the San Juan Basin and on the Laramie farther to the west
near Durango and elsewhere.
1877. MACFARLANE, JAMES: Coal regions of America, their topography,
geology, and development, xvi, 676 pages, 25 maps, New York,
1783, 2d edition; New York, 3d edition, xvi, 700 pages, maps,
plates. New York, 1877.
BIBLIOGRAPHY AND NOTES 669
No. Date.
(Pp. 72-76) The author describes the coal beds of the Cer-
rillos field, and mentions those of the Rio Puerco and other
New Mexico fields.
48. 1877. WHITE, CHARLES A.: Report on the invertebrate fossils collected
in portions of New Mexico and Arizona by parties of the expe-
ditions of 1871, 1872, 1873, and 1874. United States geographical
surveys west of the 100th meridian, in charge of Wheeler, Re-
ports, vol. 4, paleontology, part 1, 219 pages, plates 1-21, 4°.
Washington, 1877.
Abstract, Am. Jour. Sci., 3d series, vol. 12, pp. 62-63 (4% p.).
1876.
The Cretaceous is not subdivided in this report. Several of
the fossils described are from the Rio Puerco and neighboring
regions.
49. 1878. LESQUEREUX, LEO: “The lignitic formation of North America” and
“Descriptions of the Tertiary fossil plants.”
United States geological and geographical survey of the Ter-
ritories, F. V. Hayden in charge. Contributions to the fossil
flora of the western Territories, parts 1 and 2, the Tertiary
flora, by Leo Lesquereux, pp. 3-366, 15 oe 4°. Washington,
1878.
Reviewed by E. D. Cope, Am. Nat., vol. 42, pp. 243-246. 1878.
(P. 314) The fossil plants from Placiére (Cerrillos field) are
included in the Tertiary flora. They are Palmocarpon compo-
situm Lx.; Carpites ligatus Lx.; Palmocarpon mexicanum Lx.;
Carpites spiralis Lx.
The formation (the Mesaverde of the Cerrillos field) is
placed in the “first group,” together with those in the Raton,
Canyon City, Denver, and other coal fields.
50. 1879. Copr, Epwarp D.: The relations of the horizons of extinct Verte-
brata of Europe and North America.
United States geological and geographical survey of the Ter-
ritories, F. V. Hayden in charge, Bull., vol. 5, pp. 33-54. Wash-
ington, 1879.
(P. 50) Puerco (?) is shown as occurring above Laramie.
(P.52) The Puerco marls first observed by Cope in 1874 were
referred by Endlich in 1875 “to the lowest place in the Tertiary
series, but the absence of fossils renders it difficult to conclude
whether they belong here or in the Laramie series.”
51. 1879. STEVENSON, JOHN J.: Geology of Galisteo Creek, New Mexico.
Am. Jour. Sci., 3d series, vol. 18, pp. 471-475. 1879.
(P. 471) The coal beds north of Placer Mountain (Cerrillos
field) are referred to the Laramie, and the underlying shale ex-
posed near the town of Galisteo to the Pierre, Niobrara, and
Benton.
The Galisteo sandstone is described as lying unconformably
on beds ranging from “Laramie” to Dakota. (This probably is
not the Galisteo of other writers. )
670 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No. Date.
52. 1881. StevENSON, JOHN J.: Note on the Laramie group of southern New
Mexico. Am. Jour. Sci., 3d series, vol. 22, pp. 370-372. 1881.
(P. 870) The statement is made that the “Laramie” beds are
practically continuous from Galisteo Creek southward for 150
miles. (This is an error probably arising from the fact that
coal occurs near a “San Pedro,” about 10 miles south of the
Galisteo, and also near another “San Pedro,” about 150 miles
to the south. The coal near San Pedro and San Antonio re-
ferred to by J. M. Robinson, whom Stevenson quotes, is prob-
ably the coal of the Tijeras field, but it is not certain how
much of the description refers to this field and how much to
the Carthage field near the “San Pedro” farther to the south.)
(P. 371) Ostrea congesta was observed “high up in the Lara-
mie” of the Cerrillos field, and Ostrea glabra, Anomia, Corbula
8 species, Camptonectes ?, and Tellina ? were obtained from the
coal measures near San Pedro (probably from the ceo field )
and identified by R. P. Whitfield.
53. 1881. Stevenson, JOHN J.: Report on geological examinations in south- ©
ern Colorado and northern New Mexico during the years 1878
and 1879. United States geographical surveys west of 100th
meridian, in charge of G. M. Wheeler, Reports, vol. III, Supp.,
420 pages, plates, 3 maps, 4°. Washington, 1881.
(Pp. 126-180) The “Galisteo coal field” (Cerrillos field) is
briefly described and a detailed section of the coal-bearing rocks
near the “‘western edge of area” is given, and the coal-bearing
rocks are referred to the Laramie.
(P. 1382) The subdivisions of Lower, Middle, and Upper Cre-
taceous are adopted, but Upper Cretaceous is here made equiva-
lent to No. 5 (Fox Hills) and a part of No. 4 (Pierre), and
Middle Cretaceous is made to include part of No. 4 On the
maps Middle Cretaceous is labeled Colorado. .
(P. 183) The coal beds of the Galisteo area are correlated
directly with those of southern Colorado (Trinidad field) and
with those of northern Colorado (Denver field) and Wyoming.
(P. 145) The writer states that Newberry regarded the coal
beds near Chama and farther to the north and west as younger
than those of the “Galisteo coal beds.”
(P. 145) The Galisteo coal beds are correlated with New-
berry’s Upper Cretaceous of the Chama region (Newberry him-
self had referred them to Middle Cretaceous).
Cope’s description of the rocks near Chama in the Wheeler
reports (Nos. 26 and 36 of this list) is quoted as proof that
Cope was describing the Upper Cretaceous of Newberry. Ste-
venson uses this for correlating with his Laramie. (P. 155)
Inoceramus and Ostrea were found in the “Laramie” of the
Galisteo area.
(Pp. 159-162) The Galisteo sandstone is referred to the Ter-
tiary. (The description and the mapping indicates that the
writer’s Galisteo is quite different from the Galisteo of other
No.
D4.
56.
oT.
58.
59.
BIBLIOGRAPHY AND NOTES 671
Date.
authors and probably younger, for it lies with marked uncon-
formity on older rocks. The Galisteo sandstone of other authors
is evidently regarded as a part of Stevenson’s “Laramie;” see
author’s figure 49.) (Pp. 328-346) Detailed descriptions and
sections of the coal-bearing rocks are given.
1881. STEVENSON, JOHN J.: United States geographical surveys west of
the 100th meridian, Atlas. 1881.
For geology of New Mexico localities see Atlas sheets Nos.
oo( 5), 69(D);; TOCA) 10(C),; “17 CB), TCD).
1882. Cope. Epwarp D.: The Tertiary formation of the central region
of the United States. Am. Nat., vol. 16, pp. 177-195, plate. 1882.
The coal beds near Gallinas Mountains, New Mexico, are
mentioned (p. 180) and a section farther north, including the
coal measures, near the Colorado-New Mexico line, is described
(p. 181).
1882. STEVENSON, JOHN J.: Notes on the coal field near Canyon City,
Colorado. Am. Phil. Soc., Proc., vol. 19, pp. 505-521. 1882.
Abstract, Am. Jour. Sci., 3d series, vol. 23, p. 152 (% p.).
1882.
Brief reference is made to the coal measures on Galisteo
Creek (Cerrillos field).
1885. Copr, Epwarp D.: The Vertebrata of the Tertiary formations of
the West, book 1, United States geological survey of the Terri-
tories, F. V. Hayden in charge, Report, vol. 3, xxxv, 1009 pages,
75 plates, 4°. Washington, 1884.
Reviewed, Science, vol. 5, pp. 467-469. 1885.
(P. 42) In the table of formations Puerco and Laramie are
included under post-Cretaceous, although it is stated (p. 4)
that the Puerco belongs to the “Tertiary rather than the post-
Cretaceous,” and Fox Hills is’ used as a group name to include
“Wort Pierre” and “Fox Hills” proper. A cross-section west of
Gallinas Mountains is given, showing “lignite” below “Fox
ailis.”
1885. Cope, Epwarp D.: Relations of the Puerco and Laramie deposits.
Am. Nat., vol. 19, pp. 985-986. 1885.
Observations from David Baldwin’s notes are quoted, supple-
menting previous observations by the writer and others. The
Laramie is said to overlie the Fox Hills, to be 2,000 feet thick
at Animas City, New Mexico, and to contain characteristic
Dinosaurs. The Puerco overlies the Laramie with apparent
conformity, but is faunally distinct. It is sometimes included
with the Laramie in post-Cretaceous series.”
1885. DutTon, C. E.: Mount Taylor and the Zuni plateau. U. S. Geol.
Sury., J. W. Powell, Director, 6th Annual Report, 1884-’85, pp.
106-198, plates 11-22. Washington, 1885.
Abstracts, Am. Jour. Sci., 3d series, vol. 34, pp. 155-157, 1887;
Science, vol. 10, pp. 317-318, 1887.
672 wW.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No. Date.
The Cretaceous is not subdivided for purposes of mapping in
this paper. Observations were extended eastward to include a
part of the valley of the Rio Puerco, but attention is directed
principally to the igneous rocks, and little information is given
as to the sedimentary formations of this valley.
60. 1885. STEVENSON, JOHN J.: Some notes respecting metamorphism. Am.
Phil. Soc., Proc., vol. 22, pp.- 161-166. 1885.
Abstract, Am. Jour. Sci., 3d series, vol. 29, p. 414 (4% p.).
1885.
(P. 166) Brief reference is made to the anthracite coal of
Placer Mountain (Cerrillos field) and to the metamorphosed
coal near Trinidad and near Raton.
61. 1886. WuHite, CHartes A.: On the relation of the Laramie molluscan
fauna to that of the succeeding fresh-water Eocene and other
groups. U. S. Geol. Surv., Bull., No. 34, pp. 391-442, 5 plates.
Washington, 1886.
Abstracts, Science, vol. 10, pp. 126-127, 1888; Popular Sci.
Monthly, vol. 33, p. 420 (44 col.), 1888.
The relation of Laramie and Puerco is discussed and some
of the invertebrates from the Puerco near Nacimiento are de-
scribed.
62.' 1889. STEVENSON, JoHN J.: The Mesozoic rocks of southern Colorado
and northern New Mexico.
Am. Geol., vol. 3, pp. 3891-897. 1889.
(Pp. 891-892) The coal-bearing rocks of the Canyon City,
Trinidad, Raton, and Galisteo (Cerrillos) coal fields are re-
ferred to the Laramie. Rocks of Fox Hills age are supposed to
occur below the coal near Canyon City and Trinidad, Colorado,
but to thin out farther to the south and are “supposed to be
absent” in the Galisteo area.
63. 1890. Corr, Epwarp D.: (Remarks on the age and stratigraphic com-
ponents of the Laramie group.)
Geol. Soc. Am., Bull., vol. 1, p. 582, 1890; Am. Nat., vol. 24, p.
569, 1890. :
The Puerco containing “about 100 species of mammalia” is
said to rest on the Laramie, which also contains some mammals.
64. 1890. NEwBeRRY, JoHN S.: The Laramie group. Its geologic relation,
its economic importance, and its fauna and fiora.
New York Acad. Sci., Trans., vol. 9, pp. 27-32. 1890.
Abstract (by author), Geol. Soc. Am., Bull. vol. 1, pp. 524-
527, 527-528, 1890, with discussion by J. B. Tyrrell, L. F. Ward,
J. J. Stevenson, and E. D. Cope, a5 527-532.
Other abstracts, Am. Geol., vol. 5, pp. 118 (44 p.); Am. Nat.
vol. 24, pp. 856-857 (44 p.).
The coal beds of New Mexico enter into the discussion only
incidentally. ¥
65. 1890. Stevenson, JoHN J.: (Remarks on the differentiation of the Colo-
rado group in Colorado and New Mexico.)
BIBLIOGRAPHY AND NOTES 673
No. Date.
Geol. Soc. Am., Bull., vol. 1, p. 532 (4% p.), 1890; Am. Nat.,
vol. 24, pp. 568-569, 1890.
Discussion of paper by J. S. Newberry, “The Laramie group.”
The writer states that the Fox Hills thins out to the south
in New Mexico, but that the other Cretaceous formations con-
tinue around the mountains to the Rio Grande. (These forma-
tions are not known to exist over a large area at the southern
end of the mountains. )
66. 1890. Warp, Lester F.: (Remarks on the age of the Laramie group.)
Geol. Soc. Am., Bull., vol. 1, pp. 529-532, 1890; Am. Nat., vol, 24,
pp. 564-568, 1890. :
Discussion of paper by J. S. Newberry on “The Laramie group.”
Discussion in which the coal beds of New Mexico are as-
sumed to be Laramie.
67. 1893. EMMons, SAMUEL FRANKLIN: Excursion to the Canyon of the
Colorado. Itinerary, Denver, Colorado, to Albuquerque, New
Mexico.
Int. Cong. Geol., Compte Rendu, 5th session, pp. 464-468. 1895.
The reference of the coal beds near Ortiz in the Cerrillos
field to Laramie is accepted.
68. 1895. Osporn, H. F., and Eartr, CHARLES: Fossil mammals of the
Puerco beds. Am. Mus. Nat. Hist., Bull., vol. vii, pp. 1-70, figs.
1-21. 1895.
The coal beds below the Puerco are assumed to be Laramie,
and the Puerco is said to contain “several Laramie reptiles”
(p. 4).
69. 1896. STEVENSON, JOHN J.: The Cerrillos coal fields near Santa Fe, New
Mexico. N. Y. Acad. Sci., Trans., vol. xv, pp. 105-122. 1896.
Abstract, Geol. Soc. Am., Bull., vol. vii, pp. 525-527; Science,
new ser., vol. iii, pp. 392-394. 1896.
(P. 111) The statement is reiterated that the Fox Hills stage
of the Rocky Mountain region is not represented in this area
and the coal beds are assumed to be Laramie. Sections of the
coal-bearing rocks are given, the characteristics of the coal de-
scribed, and several analyses of the coal are given. The meta-
morphosis of the bituminous coal into anthracite is discussed.
70. 1897. FtemMine, JoHN W.: (Coal mines of New Mexico.) Report of the
Governor of New Mexico to the Secretary of the Interior.
Washington, 1897, pp. 91-115.
The report contains a geologic section of the rocks exposed
near Madrid in the Cerrillos coal field. Coal mines in northern
New Mexico near Monero are referred to.
71. 1898. FLemMinc, JoHN W.: (Coal mines of New Mexico.) Report of the
Governor of New Mexico to the Secretary of the Interior.
Washington, 1898, pp. 56-86.
The report contains a geologic section of rocks iiuien near
Madrid in the Cerrillos coal field.
674 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No. Date.
The mines at Monero are described, where three beds of coal
ranging in thickness from 3 feet 6 inches to 3 feet 10 inches
have been opened.
72. 1898. Herrick, C. L.: The geology of the San Pedro and the Albuquerque
districts (New Mexico).
Denison Univ., Sci. Lab., Bull., vol. xi, pp. 93-116, pl. xiii.
1898.
The coal-bearing rocks outcropping on the Rio Puerco (p. 97)
and those of the Tijeras field (pp. 108-109) are described as
Cretaceous.
(P.112) The coal beds of the Cerrillos field at Waldo, Madrid,
and Omera are briefly mentioned. A sketch map of the geologic
formations accompanies the paper.
73. 1898. SPENCER, ARTHUR CoE: The Upper Cretaceous section in south-
western Colorado. Abstract, Science, new ser., vol. vi, p. 143
(% p.). 1898.
The statement is made that above the Dakota “comes a series
of shales, known to embrace the Benton, Niobrara, and a part
of the Pierre, which can not be divided on lithologic grounds.
The upper part of the section . . . consists of massive sand-
stones in which both the Fox Hills equivalent and that of the
Laramie may prove to be present.” No mention is made of the
Lewis shale.
74. 1899. FLemMiInG, JOHN W.: (Coal mines of New Mexico.) Report of the
Governor of New Mexico to the Secretary of the Interior.
Washington, 1899, pp. 164-209.
The coal mines near Madrid in the Cerrillos field are de-
scribed and the geologic relations of the coal beds shown by
columnar section.
The mines at Monero are also described.
75. 1899. Cross, WHITMAN: U.S. Geol. Survey, Geol. Atlas of U. S., folio
No. 60. 1899.
(Pp. 4 and 5) The coal-bearing rocks are described as the
Mesaverde formation and are underlain by Mancos shale and
overlain by Lewis shale.
(P. 4) The Lewis is described as about 2,000 feet thick. The
occurrence of coal-bearing rocks above the Lewis is noted, but
doubt is cast on their assignment to the Laramie.
(P. 5) The lower part of the Mancos shale contains the fol-
lowjng characteristic Benton fossils: Gryphea newberryi; Os-
trea lugubris; Ostrea congesta; Inoceramus labiatus; Inocera-
mus fragilis; Inoceramus dimidius; Prionocyclus macombdi;
Baculites gracilis; Scaphites warreni; Anatina sp.?; Plicatula
n. sp.
The upper part of the Mancos contains the following Pierre
fossils (this revised list has been prepared for the present paper
by T. W. Stanton): Jnoceramus barabini; Inoceramus sp.3
Inoceramus sagensis; Syncyclonema rigida; Scaphites sp.;
BIBLIOGRAPHY AND NOTES 675
No. Date.
Baculites sp., a large form resembling Baculites ovatus or
Baculites compressus; Arca sp.?; Turritella sp.?
76. 1900. FLemine, JoHN W.: Report of the mine inspector for the Tertiary
of New Mexico.
Report of the Governor of New Mexico to the Secretary of
the Interior. Washington, 1900, pp. 279-314.
The mines of the Cerrillos coal field are described and those
of Monero are mentioned.
77. 1900. Herrick, C. L., and Jonnson, D. W.: The geology of the Albu-
querque sheet (New Mexico).
Denison Univ. Sci. Lab., Bull., vol. xi, art. ix, pp. 175-239, pls.
XxVii-lviii. 1900.
Hadley Lab. Univ. of New Mexico, Bull., vol. ii, pt. i, 1900,
pp. 1-67, 32 pls., colored geologic map in pocket. 1900.
(Pp. 187-188) A Gastropod zone is described as occurring
about 40 feet above the Dakota sandstone, followed upward by
the Tres Hermanos sandstone and a Concretion zone, which
“abounds in large ammonites shells and large species of Pinna
and Baculites.’ This zone was recognized, according to these
writers, near Cabezon, about 20 miles to the northwest and
near Una del Gato (Hagan field), about 30 miles to the east.
These three zones are close together, and from them, in the Rio
Puerco, Hagan, and Tijeras fields, the following fossils were
collected: [It is not always possible to determine from the de-
scriptions when the authors refer to the Concretion zone and
when to the Cephalopod zone. Hence it is possible that some of
the following species may have come from the Cephalopod
zone.| Ostrea translucida M. & H.; Exogyra leviscula Roemer ;
EHxogyra columbella Meek; Mactra(?) subquadrata H. & J.;
Tapes cyrimeriformis Stanton; Caryates veta Whitfield; Phola-
domya subventricosa M. & H.; Liopistha concentrica Stanton;
Camptonectes symmetricus H. & J.; Dosinia sp.; Chemnitzia
sp.; Sigaretus textilis Stanton; Baculites gracilis Shumard ?;
Prionotropis woolgari Mantell; a thick shale (the principal
part of the Mancos) occurs above the Concretion zone, but its
thickness is not given. Apparently the space occupied by it is
represented by the hiatus in the section east of Prieta Mesa,
given in plate 22. (Johnson has stated personally to the present
writer that the shale between the ‘Concretion zone’ and the
“Cephalopod zone’ was roughly estimated at 1,000 feet.) A
Cephalopod zone occurs about 100 feet from the top of this
shale (the present writer found this zone to be about 300 feet
from the top), and above it occurs the Punta de la Mesa sand-
stone—the basal member of the yellow sandstones described as
the “Prieta Series.” These sandstones, together with the Cepha-
lopod zone, are referred to the Fox Hills. [The sandstones are
now referred to the Mesaverde and the Cephalopod zone to the
Benton.] From them the following fossils were identified:
Ostrea lugubris Conrad; Ostrea sannionensis White; Gryphea
676 WwW. T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
78.
79.
80.
81.
Date.
vesicularis Lam.; Inoceramus fragilis H. & M.; Pinna petrina
White; Rostellites anbigua Stanton; Buchiceras swallovi Shu-
mard; Sphenodiscus lenticulare Owen; Placenticeras placenta
De Kay; Placenticeras costata H. & J.; Pholadomya subventri-
cosa; Scaphites nodosus M. & H.; Scaphites sp. [The descrip-
tion of locality is vague. The Scaphites probably are from
near the middle of the Mancos shale. ]
The upper part of the “Prieta series” contains marine shells
said to be of Fox Hills age and fossil plants “not identifiable
with familiar Laramie species.” The following fossils were
collected from these coal-bearing rocks in the Rio Puerco,
Hagan, and Tijeras fields: Ostrea prudentia White; Ostrea
franklini Coquand ?; HLaogyra texana Roemer; Exogyra win-
chelli White; Mactra pulchella H. & J.; Tellina(?) perlata
H. & J.; Tellina equilateralis Meek; Idonarca(?) depressa
White; Cardium pauperculum Meek; Cardium sp.; Legumen
(?) oppressum Conrad; Chemnitzia coalvillensis Meek; Gyrodes
depressa Meek; Pyropsis bairdi M. & H.; Rostellites dalli Stan-
ton; Valutomorpha (?) nova-mexicana H. & J.; Harpa(?) oc-
cidentalis H. & J.; Baculites asper Morton; shark’s teeth; plants.
(P. 17) Tertiary beds “with remains of vertebrates which we
presume to be representatives of lower Tertiary strata” lie
stratigraphically above the coal-bearing rocks on the Rio Puerco.
1900. Herrick, C. L.: Report of a geological reconnaissance in western
Socorro and Valencia counties, New Mexico.
Am. Geol., vol. xxv, pp. 331-346, pls. vili-lx. 1900.
This paper supplements to some extent the information given
in the description of the Albuquerque sheet (p. 338). A section
measured east of Prieta Mesa is given, in which the Cephalopod
zone is placed only about 100 feet above the Tres Hermanos
sandstone (this Cephalopod zone seems to be the Concretion
zone of Herrick and Johnson). The coal-bearing sandstones
and shales (Mesaverde) are about 1,600 feet thick and are
overlain by Tertiary.
1901. Herrick, C. L.: Applications of geology to economic problems in
New Mexico. Int. Mg. Cong., 4th session, Proc., pp. 61-64. 1901.
(P. 64) Attention is called to the fact that some of the New
Mexico coal-bearing rocks formerly supposed to be Laramie
contain Ostrea glabra and are overlain by marine Cretaceous
beds “with fossils like those of the upper Fox Hills group.”
1901. SHERIDAN, Jo E.: Report of the mine inspector for the Territory
of New Mexico.
Report of the Governor of New Mexico to the Secretary of
the Interior. Washington, 1901, pp. 309-351.
The coal mines of the Cerrillos field and those at Monero are
‘described.
1902. Ler, W. T.: The Morrison shales of southern Colorado and north-
ern New Mexico.
Se LS os lh OU mC DC UmrheemhUC CCU UC UL
‘
BIBLIOGRAPHY AND NOTES 677
Jour. Geol., vol. 10, pp. 36-58, 7 figs. 1902.
The Exeter sandstone is named and described in this paper.
1902. Storrs, L. S.: The Rocky Mountain coal fields. U. 8S. Geol. Surv.,
22d Ann. Rept., pt. 3, pp. 415-471, 2 pls., 1 fig. 1902.
The coal beds of the San Juan Basin and of the Cerrillos and
Hagan fields are referred to the Laramie and the coal of the
latter two is said to lie ‘“‘under the Tertiary beds.”
1903. JoHNson, D. W.: Geology of the Cerrillos Hills, New Mexico.
Part I, General geology; part II, paleontology; part III, petrog-
raphy.
School of Mines Quart., vol. 24, pp. 303-350, 7 pls., 7 figs.; pp.
456-500, 10 pls,, 6 figs,, 1903; pp. 173-246, 14 pls., 19038; vol. 25,
pp. 69-98, 5 pls., 1903.
The reports result from the work done in 1899-1902. Among
others the following propositions are supported :
(1) The Santa Fe marls of Hayden . . . represent the
time from the early Loup Fork Tertiary to the Recent period.
(2).The Galisteo Group of Hayden consists of red beds of
late Cretaceous, probably Laramie age.
(38) The coal series, or Madrid Group, is of Fox Hills age.
(4) Pierre, Benton, and probably Dakota and Jura-Triassic
beds, are also present in the district.
(Vol. 24, pp. 336-338) The Galisteo sandstone is referred
doubtfully to the Laramie and is described as consisting of red
sedimentary rocks similar lithologically to the older “Red
Beds,” and lying conformably (? see discussion on this point in
the present paper) on the Madrid group. They contain fossil
wood which, according to F. H. Knowlton, indicates a species
of Quercus and is evidently of Upper Cretaceous or later age.
(Pp. 338-344) The Madrid Coal Group is described as 1,500
to 2,000 feet thick. The coal is said to be in the lower part of
this group. The author’s figure 5 makes the base of the group
rest on the lowest sheet of intrusive igneous rock at Madrid
and places the rocks below this sheet in the Pierre. (This
would place in the Pierre below the Madrid group a considerable
thickness of sandstone and several thin beds of coal which
obviously belong in the Madrid or coal-bearing formation.)
The base of the Madrid group is obviously drawn but little
below the coals that have been mined, for the writer states
(p. 340) that “the coal in the lower portion of the Madrid
group has proven of great interest to geologists, and so many
references have been made to it,” etcetera.
(Pp. 344-347) The Pierre group is described as consisting of
shale and sandstone. A section’ (p. 346) places 162 feet of
sandstone above the dark-colored shale (Mancos) in the Pierre.
(P. 347) No undoubted Niobrara was found, but the Benton
and Dakota occur.
(Pp. 477-493) The economic features of the coal are described.
Fossil leaves, identified by Knowlton (p. 178, Paleontology) as
678 W.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
84.
Date.
Ficus rhamroides Knowlton, Ficus uncata Lesquereux, Quer-
cus ? sp., and Aralia? sp. were found above the highest coal
bed east of Madrid.
In some places fossils characteristic of the Colorado and Mon-
tana groups seem to occur together (p. 182) as follows: Jno-
ceramus labiatus Schloth. (Colorado form); WStantonoceras
pseudocastatum Johnson (Colorado form); Astarte evansi H.
and M. (Montana form) ; Placenticeras placenta De Kay (Mon-
tana form) ; Baculites anceps Lamarck.
At another locality (p. 183) Ostrea lugubris Conrad (Colorado
form) and Astarte evansi H. and M. (Montana form) were
found together.
The following faunas of the Cerrillos region are described:
Pierre fauna—Lingula subspatulata H. and M.; Ostrea anomii-
oides var. nanus Johnson; ? Ostrea congesta Conrad; Inocera-
mus simpsoni Meek; Inoceramus vanuxemi M. and H.; Inocera-
mus balchii M. and H.; Inoceramus cripsi var. barabini Morton;
Inoceramus irregularis Johnson; Jnoceramus sp.; Endocostea
typica Whitfield; Endocostea brooksi Johnson; Arca madriden-
sis Johnson; Trigonarea obliqua Meek; Nucula subplana M.
and H.; Astarte evansi (H. and M.) Whitfield; Protocardia
rara E. and §8.; Cyprimeria ? sulcata Johnson; Solen cuneatus
Gabb; Corbula mematophora var. fitchi Johnson; Natica sp.;
Turritella galisteoensis Johnson; Rostellario ? terana Conrad;
Tritonium kanabense Stanton; Admetopsis ? elevata Johnson;
Helicoceras pariense White; Baculites anceps Lamarck; Bacu-
lites sp.; Placenticeras placenta De Kay; Placenticeras ? sp.;
Placenticeras ? intermedium Johnson; Placenticeras ? rotunda-
tum Johnson; Stantonoceras guadaloupe Roemer; Beryx sp.
Benton fauna—Ostrea lugubris Conrad; Inoceramus fragilis
H. and M.; Jnoceramus labiatus Schloth.; Inoceramus dimidius
White; Znoceramus strongi Johnson; Acmea cerrillosensis John-
son; Seurria coniformis Johnson; Rostellites dalli var. wellsi
Johnson; Rostellites ambigua Stanton; Prionocyclus wyoming-
ensis Meek; Prionocyclus macombi Meek; Prionocyclus sp.;
Prionotropis woolgarit Mantell; Scaphites warrent M. and H.;
Beryz sp.; Baculites anceps Lamarck; Stantonoceras pseudo-
costatum Johnson.
1903. REAGAN, ALBERT B.: Geology of the Jemez-Albuquerque region,
New Mexico. Am. Geol., vol. 31, pp. 67-111, 7 pls. 1903.
See also Ind. Acad. Sci., Proc., pp. 187-198. 1903.
A geologic sketch map, showing the distribution of the forma-
tions from Cabezon eastward to Hagan, is given.
(P. 79) The author’s Fox Hills includes the sandy rocks below
the coal; and the. coal-bearing rocks, 500 feet thick, are de-
scribed as “Fort Union” or “Laramie.” His “Fox Hills” and
“Fort Union’ constitute the “Fox Hills’ of Herrick and John-
son and the Mesaverde of later writers.
86.
87.
88.
89.
90.
91.
92.
Date.
1904.
1904.
1904.
1904.
1904.
1905.
1905.
1905.
BIBLIOGRAPHY AND NOTES 679
(P. 81) The colored sediments lying unconformably on the
coal-bearing rocks south of San Isidro (in the Rio Puerco field)
are referred to the Puerco.
JONES, FAYETTE ALEXANDER: New Mexico mines and minerals.
World’s Fair edition, 1904. Santa Fe, New Mexico, the New
Mexican Printing Company, 1904. 349 pp., 50 figs.
(P. 7) The New Mexico coal beds are referred to Fox Hills
and Laramie. The coal of the Cerrillos field is referred to the
Fox Hills.
KEYES, CHARLES ROLLIN: Unconformity of the Cretaceous on older
rocks in central New Mexico. Am. Jour. Sci., 4th ser., vol. 18,
pp. 360-362, 2 figs. 1904.
_ Cretaceous sandstone (2,000 feet thick) lying above rocks of
Montana age (presumably the coal-bearing sandstones described
in this paper as Mesaverde) are referred to the Laramie.
KEYES, CHARLES ROLLIN: The Hagan coal field (New Mexico).
Eng. & Mg. Jour., vol. 78, pp. 670-671, 3 figs. 1904.
The Hagan coal field is described with sketch maps and geo-
logic sections. A detailed section is given of the coal-bearing
rocks measured at the Hagan mine.
SHERIDAN, JO H.: Annual report of the mine inspector for the Ter-
ritory of New Mexico.
U. S. Mine Inspector for the Territory of New Mexico, Ann.
Rept. to the Secretary of the Interior for the year ended June
30, 1904. Washington, 1904, 79 pp.
(Pp. 32-38) The coal beds of the Cerrillos, Una del Gato
(Hagan), and Monero fields are described.
LAKES, ARTHUR: The coal fields of Colorado.
Colo. Sch. Mines, Bull., vol. 2, no. 2, pp. 11-28, 2 figs. 1904.
Ogitvig, Ipa H.: The high altitude conoplain; a topographic form
illustrated: in the Ortiz Mountains (New Mexico).
Am. Geol., vol. 36, pp. 27-34, 1 pl. 1905.
The conoplain described lies across the eroded coal beds of
the Cerrillos and Hagan fields.
SHERIDAN, Jo EH.: Annual report of the mine inspector for the
Territory of New Mexico.
U. S. Mine Inspector for the Territory of New Mexico, Ann.
Rept. to the Secretary of the Interior for the year ended June
30, 1905. Washington, 1905.
(Pp. 40-48) Describes the Cerrillos and Una del Gato (Hagan)
coal fields. |
STANTON, T. W.: Morrison formation and its relation with the
Comanche series and the Dakota formation.
Jour. Geol. vol. XIII, pp. 657-669. 1905.
(P. 664) Some of the rocks in northeastern New Mexico and
southeastern Colorado heretofore called Dakota are shown on
fossil evidence to be Comanche.
680 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
96.
98.
100.
Date.
(P. 666) Near Canyon City, Colo., the shale which separates
the two plates of so-called Dakota sandstone was found to con-
tain a Comanche fauna.
1906. GRIFFITH, WILLIAM: Kinds and occurrence of anthracite coal.
Min. Mag., vol. 13, no. 3, pp. 214-221, March. 1906.
(P. 218) Brief reference is made to the Cerrillos coal.
1906. JoNES, FAYETTE A.: Mineral resources of New Mexico. Am. Min.
Cong., Sth Ann. Sess., pp. 135-148. 1906.
(P. 143) Brief reference is made to the coal beds of New
Mexico.
1906. KEYES, CHARLES R.: Orotaxial significance of certain unconformi-
ties. Am. Jour. Sci., 4th ser., vol. 21, pp. 296-300, 2 figs., April,
1906.
A generalized section is given showing the position of certain
unconformities in the sedimentary rocks of New Mexico (two of
which—between ‘‘Dakotan and Coloradan,” and between ‘“‘Mon-
tanan and Laramian’—affect rocks described in the present
paper, but which are not confirmed by the present writer).
1906. KryEsS, CHARLES ROLLIN: Geological section of New Mexico.
Science, new ser., vol. 23, pp. 921-922, June 15, 1906.
A generalized geologic section is given.
1906. Ler, WiLtis T.: The Engle coal field, New Mexico. U. S. Geol.
Survey, Bull. no. 285, p. 240. 1906.
The coal beds of the Engle field contain numerous plant re-
mains and rest on rocks containing a Benton fauna. Lying
unconformably on the coal-bearing rocks are red sedimentary
rocks similar in general appearance to the Galisteo sandstone of
the Cerrillos field. Triceratops bones were found in these red
rocks. The correlation of the coal with that at Cerrillos and
Raton is suggested.
1906. Merritt, GEORGE P.: Contributions to the history of American
geology. U. S. Nat. Mus., Ann. Rept. 1904, pp. 189-733, 37 pls.,
141 figs. 1906.
Several brief sketches are given of the men who worked in
New Mexico and of the results obtained by them. Chapter X is
devoted to the Laramie question.
1906. RirrerR, ETIENNE A.: Les basin lignitiferes et houillers des Mon-
tagnes Rocheuses. Annales des Mines, 10° ser., t. 10, livr. 7,
pp. 5-84. 1906.
(P.52) The Fox Hills age for the Cerrillos coal measures is
accepted.
1906. ScHRADER, FRANK CHARLES: The Durango-Gallup coal field of
Colorado and New Mexico. U. S. Geol. Survey, Bull. no. 285,
pp. 241-258. 1906. ;
A map is presented outlining the north, east, and south sides
of the principal part of the coal fields of the San Juan basin.
Five groups of coal beds are mapped: (1) a Colorado group in
the southwestern part of the field; (2) a lower Montana group—
BIBLIOGRAPHY AND NOTES 681
No. Date.
relation to the Mesaverde unknown—occurring also in the south-
western part of the field; (8) a Mesaverde group occurring on
the north and east parts of the field; (4) an “upper Montana
' group—relation to the Mesaverde unknown’—occurring in the
south and southeastern parts of the field; and (5) a “Laramie”
group occurring in the northern and northeastern parts.
The “Laramie” is shown from Colorado as far south as Gallinas
Mountains, New Mexico, and is the same as the “Laramie” of
other writers; the Mesaverde extends as far south as the Puerco
River. The upper Montana group occurs in the southeastern
part of the field near Cabezon, and is the Mesaverde of later
writers. The other groups occur only west of the area described
by the writer.
(P. 251) The Chico Arroyo district, extending from Sierra
Nacimiento to Mount Taylor, contains coal-bearing rocks 2,000 to
3,000 feet thick, which are said to lie unconformably on the
Mesaverde and to contain fossils which indicate that they are
younger than Mesaverde. These constitute the “upper Montana
coal group.” (The “Mesaverde” and the “upper Montana coal
group” of Schrader together constitute the Mesaverde of Gard-
ner and the present writer.) .
101. 1906. SHERIDAN, Jo E.: Report of the mine inspector for the Territory
of New Mexico to the Secretary of the Interior for the year
ended June 30, 1906. Washington, Government Printing Office,
1906. 87 pp.
(Pp. 51-57) The Cerrillos and Una del Gato (Hagan) coal
fields are described.
102. 1906. SHERIDAN, Jo H.: Present conditions and future prospects of the
coal-mining industry in New Mexico.
Annual Report U. S. Mine Inspector for the Territory of New
Mexico to the Governor of New Mexico, Santa Fe, 1906, 134 pp.
(Pp. 66-69) The coal mines at Monero are described. Three
beds of coal varying from 3 to 4 feet in thickness are said to be
worked.
(Pp. 70-78) The mines in the Cerrillos and Una del Gato
(Hagan) fields are briefly described.
103. 1907. CampsBeLtL, Marius R.: The Una del Gato coal field, Sandoval
County, New Mexico, U. S. Geol. Survey, Bull. no. 316, pp. 427-
430, 1 fig. 1907.
The Una del Gato (Hagan) field is described principally from
an economic point of view. A section of the rocks measured by
Charles R. Keyes near Sloan mine is given. The coals are cor-
related with those of the Cerrillos field, and the statement is
made that “it is highly probable that they are Laramie.”
104. 1907. LrEr, WILLIS T.: Note on the red beds of the Rio Grande region in
central New Mexico.
Jour. Geology, vol. 15, no. 1, pp. 52-58. 1907.
(P.57) Coal-bearing rocks near Elephant Butte, New Mexico,
682 w.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
105.
106.
107.
108.
109.
Date.
1907.
1907.
1908.
are described as underlying red beds containing bones of T'ricera-
tops, which suggest late Cretaceous age. Red beds of similar ap-
pearance near Cerrillos, New Mexico, known as Galisteo sand-
stone have also been regarded as late Cretaceous, and the cor-
relation of the two is suggested.
SHALER, MILLARD K.: A reconnaissance survey of the western part
of the Durango-Gallup coal field of Colorado and New Mexico.
U. S. Geol. Survey, Bull. no. 316, pp. 376-426, 2 pls. 1907.
The paper deals with the geology of the western part of the
San Juan Basin.
SHERIDAN, Jo E.: Report of the mine inspector for the Territory
of New Mexico to the Secretary of the Interior for the fiscal
year ended June 30, 1907.
Washington, Government Printing Office, 1907, 48 pp.
(Pp. 53-36) The coal beds of the Cerrillos and Hagan fields
are described.
. CAMPBELL, M. R.: Coal fields of the United States.
Map, with explanations. U.S. Geol. Surv. 1908.
. JONES, FAYETTE A.: Epitome of the economic geology of New
Mexico. Published by direction of the New Mexico Bureau of
Immigration. 1908. 47 pp.
Brief references are made to the coal beds.
Summer, H. W., and Bropcett, Miuprep E.: The stratigraphy of the
Mount Taylor region, New Mexico. Am. Jour. Sci., 4th ser., vol.
-25, pp. 53-67, 4 figs., January, 1908.
This paper is a report on observations made in 1906 in the
Rio Puerco Valley south of Cabezon.
(P.54) The “Gastropod Zone” near the base of the Cretace-
ous; the ‘“Concretion (Septaria) Zone” (near the Tres Hermanos
sandstone) and the “Cephalopod Zone” (near the top of the
Mancos) of Herrick and Johnson were recognized, but most of
the fossils collected are from the latter two zones, although one
fossil, Gryphea newberryi Stanton, was found below the “Sep-
taria Zone.”
(P.56) The following fossils of Benton age were collected
from the “Septaria Zone,’ about 8 miles southwest of Casa
Salazar: Placenticeras ? rotundatum Johnson; ? Prionocyclus
wyomingensis Meek; Lima utahensis Stanton; Stantonoceras
stantoni Johnson; Scaphites sp.; Turritella whitei var. stantoni
S. and B.; ? Ostrea lugubris Conrad.
(P.57) The “Septaria Zone” of these authors is said to dis-
appear under the surface a short distance north of Casa Salazar.
(This fixes its horizon near the base of the thick shale above the
Tres Hermanos sandstone. )
(P.57) About seven miles southwest of Cabezon (supposed to
be near the top of the Mancos shale), the following fossils were
collected: TJTvrigonarca depressa White; *Lucina cf. subundata
H. and M.; *Pteria linguiformis (E. and S.); **Solemya ?
BIBLIOGRAPHY AND NOTES 683
No. Date.
.obscura Stanton; Pinna sp.; **Actwon propinquus Stanton.
(Those marked * are said to be of Pierre age, and those
marked ** to be of Benton age.)
(P.58) About 16 miles southeast of Cabezon (probably near
the top of the Mancos shale) the following fossils were found:
Prionotropis woolgari (Mantell) ; Placenticeras placenta (De-
kay) ; Astarte evansi (H. & M.) Whitfield, and 7 miles farther
southeast, at about the same horizon as those named above, the
following were collected: Gryphewa newberryi Stanton; J/nocera-
mus labiatus (Schlotheim); IJnoceramus dimidius var. labia-
toides S. and B.; ? Yoldia subelliptica Stanton; Anomia propa-
toris White; Ostrea lugubris Conrad; Ostrea anomioides var.
nanus Johnson; Cardium pauperculum Meek; Turritella whitei
var. stantoni S. and B.; Lunatia concinna (H. and M.) ; Priono-
tropis hyatti Stanton; Prionotropis woolgari (Mantell).
(Pp. 59-60) Evidence is given to the effect that there are two
“Septaria zones” below the “Caphalopod zone” of Herrick and
Johnson, which contain a fauna said to be “almost totally dis-
tinct from the Septaria fauna. The authors conclude that the
strata yielding the fossils described vary in age from Benton to
doubtful Pierre and “show a commingling of many species of
the Colorado formations with a few of the Montana. This
would apparently indicate an upper Fort Benton age for the
beds unless we suppose that the apparent absence of clear water
in this region during Niobrara times would cause the absence of
the typical Niobrara fauna and the persistence of the Fort
Benton fauna to Montana times. Under such a _ supposition,
some of these intermediate strata would represent the Niobrara
time, without the presence of the typical Niobrara fauna.”
110. 1909. GARDNER, JAMES H.: The coal field between Gallina and Raton
Spring, New Mexico, in the San Juan coal region.
U. S. Geol. Survey, Bull. 341, pp. 335-351, 1 pl. (map). 1909.
Two coal-bearing formations southwest of Nacimiento Moun-
tains are described. They are the Mesaverde, which includes
Schrader’s “Upper Montana Group,” and the “Laramie.” These
— are separated by Lewis shale, which is said to be 2,000 feet thick
near Gallina and only 250 feet thick on the Arroyo Torreons, about
30 miles to the southwest. Several geologic sections are given
showing the relations of the coal beds to other rocks.
(P. 338) “At a point 10 miles north of Gallina a part of the
(Mancos) becomes arenaceous and forms a hogback in the shale
valley. This sandy bed is about 30 feet thick and.about 275 feet
below the top of the formation. It is no doubt the beginning of
the sandstone and shale formation that increases in thickness
toward the south and is coal-bearing on the south side of the
(San Juan) basin.”
111. 1909. Ler, Wituis T.: Unconformity in the so-called Laramie of the
Raton coal field, New Mexico.
XLVIII—BuLtu. Grou. Soc. AM., Vou. 23, 1911
684
No.
113.
114.
115.
W. T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
Date.
Geol. Soc. Am. Bull., vol. 20, pp. 857-368, 3 plates, 1 fig. 1909.
The paper presents evidence that the coal-bearing rocks of the
Raton field are divisible into two formations, the lower one
possibly older than Laramie and the upper one of post-Laramie
age.
1909. Ler, Wittis T.: The Manzano group of the Rio Grande Valley,
New Mexico. U. 8S. Geol. Survey, Bull. 389, pp. 5-40, 5 pls., 9 figs.
1909.
The paper includes geologic sections of the older rocks up to
and including the Dakota sandstone in the Cerrillos and Hagan
fields.
1909. Stanton, T. W.: The age and stratigraphic relations of the “Cera-
tops beds” of Wyoming and Montana.
Washington Acad. Sci., Proc., Vol. XI, pp. 239-293. 1909.
(P. 274) The paper gives the names of invertebrates from the
‘*“Taramie” of southwest Colorado.
1910. DaRTON, NELSON Horatio: A reconnaissance of parts of north-
western New Mexico and northern Arizona.
U. S. Geol. Survey, Bull. 435, 88 pp., 17 pls., 8 figs. 1910.
The geology along the Santa Fe Railway from Albuquerque
westward is described. The Cretaceous consists of the following
formations, given in descending order: Laramie, coal-bearing ;
Lewis shale; Mesaverde, coal-bearing ; MZancos shale, locally coal-
bearing; Dakota sandstone.
(P.58) Gardner’s results are accepted for the Nacimiento
region and Herrick and Johnson’s for the Rio Vuerco region.
Herrick’s section in the Rio Puerco Valley (78, p. 338) is quoted
with several changes, and the reference of the coal-bearing rocks
including the ‘Punta de la Mesa sandstone” to the Fox Hills is
accepted. ;
A section of rocks exposed at Laguna, west of the Rio Puerco
coal field, was measured. The following fossils occur about 550
feet above the base of this section: Exrogyra columbella Meek;
Gryphea sp., probably a variety of Gryphaa newberryi; Avicula
gastrodes Meek ?; Cardium, Panopea, Turritella, Rostellites, and
F'usus sp.
About 100 feet lower in the section the following species were
collected: Haxogyra columbella Meek; Pecten sp.; Pinna petrina
White; Znoceramus ?, Leda, Cardium, and Lucina ? sp.; Tsocardia
n. sp.; Cyprimeria ? sp.. Corbula sp.; Liopistha (Psilomya)
concentrica Stanton; Turritella whitei Stanton; Tritonium kano-
bense Stanton; Actwon, Cinulia, Turrilites ?, or Heteroceras sp.
Doctor Stanton is quoted as reporting that these fossils indicate
a horizon in the Benton formation.
1910. GARDNER, JAMES H.: Isolated coal fields in Santa Fe and San
Miguel counties, New Mexico.
U. S. Geol. Survey, Bull. 381, pp. 447-451. 1910.
j
r
2
4
|
BIBLIOGRAPHY AND NOTES 685
No. Date.
A part of this paper is devoted to the “Omara Coal Field,” and
the coal beds at the Omara mine are correlated with those near
Madrid. (These localities are at opposite extremities of the
Cerrillos field.)
116. 1910. GARDNER, JAMES H.: The coal field between San Matev and Cuba,
New Mexico. U. S. Geol. Survey, Bull. 381, pp. 461-473, 1 pl.
(map). 1910.
The coal-bearing formations of the southeastern part of the
San Juan Basin are described as Mesaverde and “Laramie.” A
detailed section of the Mesaverde on Arroyo Torreons (p. 470)
shows a thickness of 1,328 feet.
The statement is made (p. 462) that the Mesaverde “is now
known to encircle the San Juan Basin. The same is true of the
overlying conformable Lewis shale and ‘Laramie’ formation.”
117. 1910. GARDNER, JAMES H.: The Puerco and Torrejon formations of the
: Nacimiento group. Jour. Geology, vol. 18, no. 8, pp. 702-741, 3
pis. S fies. - 1916.
The Tertiary and late Cretaceous formations of the San Juan
Basin west of Nacimiento Mountains are described.
The Tertiary beds rest unconformably on the “Laramie,” and
the Mesaverde coal measures are separated from the “Laramie”
by the Lewis shale.
118. . 1910. LinpGREN, WALDEMAR; GRATON, Lous C., and Gorpon, CHARLES H.:
The ore deposits of New Mexico.
U. S. Geol. Survey, Prof. Paper 68, 361 pp., 22 pls., 33 figs.
1910.
Brief references are made in many places to the coal-bearing
formations of New Mexico.
119. 1911. Lee, Wriiuis T.: Further evidence of an unconformity in the so-
called Laramie of the Raton coal field, New Mexico. (Abstract.)
ibulis.Geok ‘soc, Am:,.Vol. 22, p. T1LT... 1911.
The unconformity separating the coal-bearing rocks of the
Raton coal field into a possible pre-Laramie and a post-Laramie
formation was traced around the Raton and Trinidad coal field.
120. ——. Lee, WILLIs T.: Correlation of rocks in the isolated coal fields
around the southern end of the Rocky Mountains in New Mexico.
(The preliminary announcement of the results contained in
this paper was made at the Washington meeting of the Geo-
logical Society of America, 1911.)
121. 1912. Stosr, G. W.: The Apishapa folio, Colorado. (In press.) U. S.
Geol. Surv., Geol. Atlas U. S. No. 191.
The shale separating the two plates of so-called Dakota sand-
stone and the lower plate of this sandstone are referred on fossil
evidence to Comanche. The upper plate of sandstone is referred
to Dakota.
122. 1912. Ricuarpson, G. B.: The Monument Creek group. Bull. Geol. Soc.
Am., vol. —, pp. —. 1912. (In press.)
686 W.T. LEE—STRATIGRAPHY OF COAL FIELDS OF NEW MEXICO
No.
Date.
Dawson arkose is a name applied by this writer to the lower
part of rocks-formerly called Monument Creek. He states that
“it is evident that in the Castle Rock region the Dawson arkose,
‘together with its associated unconformities, represents the time
between the Laramie and the Oligocene . . . the lower part
of the Dawson arkose seems to pass along the strike into the
Arapahoe and Denver formations; that the Dawson and Ara-
pahoe cannot be separated lithologically, even at the type locality
of the Arapahoe on the bluffs of Willow Creek; and that the
Denver and Dawson apparently merge into each other.” It is
further stated that ‘“‘the evidence [of certain vertebrates]implies
the correlation of the lower part of the Monument Creek of
Hayden [the lower part of the Dawson arkose] and the ‘post-
Laramie’ of the Denver Basin [the Arapahoe and Denver for-
mations]. The evidence of the plants is corroborative, for .
Doctor Knowlton states that the leaves from the lower part of
the Dawson arkose . . . are undoubtedly Denver in age.”
From these statements it is evident that the Dawson is regarded
as Tertiary in age and that the Arapahoe and Denver formations
also are Tertiary.
BULL. GEOL. SOC. AM.
PRELIMINARY MAP OF PLEISTOCENE DEPOSITS OF PORTIONS OF GLACIER NATIONAL PARK AND BLACKFOOT
INDIAN RESERVATION, MONTANA
(By Wm. C. Alden, assisted by J. E. Thomas)
High mountain area dissected by many deep glaciated valleys, with small existing
Deposits of mountain glaciers of Wisconsin stage in valleys and on the plain east of
le mountai i
Deposits of the Keewatin ice-sheet of the Wisconsin stage of glaciation.
Deposits of pre-Wisconsin glacial drift capping high flat-topped ridges of Cretaceous
Bs 44 shale and sandstone—that is, lying on remnants of the Blackfoot peneplain (mapping
DOVLSX3 ~=not complete).
(Boundaries of drift of Saint Mary and Keewatin glaciers from F. H. H. Calhoun
and B. Stebinger.)
BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA
VOL. 23, PP. 687-708, PLS. 37-40 NOVEMBER 28, 1912
PRE-WISCONSIN GLACIAL DRIFT IN THE REGION OF
GLACIER NATIONAL PARK, MONTANA?
BY WILLIAM C, ALDEN
(Read before the Society December 28, 1911)
CONTENTS
Page
Existing glaciers and Wisconsin glaciation........ SE Sa yh Pe gee Le 687
EES Jean) Oae
Deposits on Two Medicine Ridge....... LG nnine Rpm PNUD Pi wiley ir 691
EE RESALE 693
Suen rise ELIVET TRIGGER. cw. ec ewe ee ewes LE A) ee ore 694
eM NAT Y PRIQEC) . . occ decent ewes cows ewan ae ee sys anesind «. 696
Deposits on ridge west of Lower Saint Mary Lake.................. 0000. 699
IIL OREIE Te OT ce vie een os cee ew cee eee wkend ca tias 699
I IRECUIPPETI FOLIP GE. ns cc cc ee ea cee ene t nate neweeneace 700
pmnpane Weermedy Ridge... ..........0. 0 cece eee | Oe eR IR ee ee 702
sore ane vicinity OF Belly River.........0.0ccceseceescwaccesccegs 704
PE Maret PEATE. 25a) 2s ois sw ak «ale ow wees boca ca wie ewes we in 705
EN ce Soci) nic ys ele wlacnisa a eels ae eu cield wee Se a atera me katie 707
EXISTING GLACIERS AND WISCONSIN GLACIATION
During the field season of 1911 the writer had the pleasure of being
associated with Mr. M. R. Campbell, Dr. T. W. Stanton, Mr. J. R.
Hoats, and Mr. J. Elmer Thomas, of the U. 8. Geological Survey, in
initiating a geological survey of Glacier National Park, Montana, his
particular assignment being the study of past and present glaciation and
associated phenomena’® (plate 37).
1 Manuscript received by the Secretary of the Society April 15, 1912.
Published by permission of the Director of the U. S. Geological Survey.
2Tt should be stated that while the surveying done by this party during the past field
season was carried on in detail wherever there was opportunity, the work as a whole
was rather in the nature of a general reconnaissance, the object being to get the various
problems in hand, but not to complete the investigation of any of them. In some re-
spects, therefore, the conclusions set forth in this paper are to be considered as tenta-
tive and subject to such modification as further studies make necessary.
The topography of Glacier Park and of the western part of the Blackfeet Indian
reservation, including the features here described, is delineated on the new topographic
map of the park and, excepting the southern part, on the Browning, Chief Mountain, and
Kintla Lake topographic sheets,
(687)
688 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
There are in the cirques at the heads of the valleys, high up on the
flanks of the mountains in the heart of the Lewis Range, one hundred or
more existing glaciers, ranging in size from those a few square rods in
extent to ice fields of 2 or 3 miles area. Besides the cirques in which
these glaciers lie, there are a multitude of glacial amphitheaters, in
many of which are beautiful lakes, but in which glaciers do not now
exist. These cirques are among the most wonderful phenomena of the
park. From these cirques broad-bottomed, steep-walled, U-shaped val-
leys extend to the mountain front, showing in their contours and in the
deposits of drift which they contain the effects of a former much more
numerous existence and much greater extension of the valley glaciers.
Numerous trunk glaciers, fed by a multitude of tributary glaciers, ex-
tended eastward and westward to and beyond the mountain front. The
deposits of those extending out on the plains to the east of the range
have been described by Mr. F. H. H. Calhoun in professional paper
number 50 of the United States Geological Survey, entitled “The Mon-
tana Lobe of the Keewatin Ice-sheet.” Ice discharging from the moun-
tain valleys tributary to Two Medicine River is described as having
coalesced and spread over the plain as “a large piedmont glacier which
extended about 50 miles from the main divide and which in its widest
part was over 30 miles across.* This is referred to as the “Blackfoot
Glacier,” a somewhat infelicitous designation, inasmuch as the largest
-of the existing glaciers in the park, but 10 miles distant from the head
of Two Medicine Valley at the nearest point, bears the name “Black-
feet.” A better name for the extinct glacier, which headed principally
in valleys tributary to Two Medicine River, would be the “T'wo Medicine
Glacier.” Perhaps I may be pardoned if on account of this conflict in
nomenclature I make this substitution. At the head of Lower Two
Medicine Lake the ice in this valley had a thickness of about 1,000 feet.
Ice in the valleys of the north and south forks of Cut Bank Creek, the
next stream north of the Two Medicine, coalesced several miles from
the mountain front forming the Cut Bank glacier, which extended about
18 miles from the Continental Divide. Two small lobes of the glacier
spilled northward through sags in the crest of Milk River Ridge* into
= hoe? Cit. 1p) LS.
4There seems to be some confusion of usage of names applied to the several ridges of
Cretaceous sandstone and shale east of the mountain front. Mr. Calhoun, in his paper,
refers to the ridge east of Lower Saint Mary Lake as “Milk River Ridge,” and to the
ridge north of Lower Two Medicine Lake as “Cutbank Ridge.” On the topographic
maps, however, the name “Saint Mary Ridge’ is applied to the ridge east of Lower Saint
Mary Lake, and the name “Milk River Ridge’ to the ridge north of North Fork of Cut-
bank Creek. This latter usage, which appears to be the common one, will be followed
in the present paper. The name “Cut Bank Ridge’ will be applied to the ridge between
= a Se
- —_- e—————
° .
oe =
EXISTING GLACIERS AND WISCONSIN GLACIATION 689
Milk River Valley, where, however, they had but relatively small exten-
sion. ‘The relations of these spillways show that the thickness of ice in
the North Fork Valley must have been about 1,000 feet just east of the
mountain front.
Saint Mary River Valley and its tributaries were occupied with ice
which formed a glacier of large size, extending northward across the
49th parallel. ‘The main stream heading, where now lie the Blackfeet
and Red Eagle glaciers, thus had a length of about 35 miles south of the
international boundary, and extended an undetermined distance north-
ward over the plain of southern Alberta. The main tributaries occu-
pied the valleys of Red Eagle, Boulder, Swiftcurrent, and Kennedy
ereeks. Glacial drift was found on the slope of Singleshot Mountain up
to 1,275 feet above the foot of Upper Saint Mary Lake, and the position
of the lateral moraine just below the crest of Saint Mary Ridge on the
east shows that the surface of the glacier stood about 1,350 feet above
the level of Lower Saint Mary Lake.
West of Chief Mountain is Belly River Valley. Heading at the Conti-
nental Divide, 10 to 12 miles south of the 49th parallel, where are now
Chaney and neighboring glaciers, a considerable stream of ice extended
northward onto the plain of southern Alberta. Still farther west a large
glacier issued from the valley west of the north end of the Lewis Range,
in which is now Waterton Lake. The extent of this stream of ice in
Alberta was not determined, but its depth is known to have been con-
siderable, for ledges smoothed and striated by this glacier were found
on the mountain slope about 1,700 feet above the head of Waterton Lake.
The fresh and unmodified character of all the phenomena resulting
from this extensive mountain glaciation indicates that it is probably to
be correlated with the last of the great extensions of the Keewatin ice-
sheet, that of the Wisconsin stage of glaciation, and this correlation is
assumed in the present discussion. The purpose of this present paper
is not, however, the discussion of this later well known glaciation, but
the description of certain deposits which indicate that the Lewis and
Livingston ranges were subjected to glaciation at another and much
earlier stage.
the north and south forks of Cut Bank Creek, and the name “Two Medicine Ridge’ to
the ridge north of Lower Two Medicine Lake. The name “Point Mt.,” which is printed
on the map on the ridge between Swiftcurrent and Boulder creeks, is applied by the
people of the region to the mountain to the southwest for which the map shows the
name “Altyn Mt.”’ It is proposed to transfer the name “Point Mt.” to this peak and to
designate the ridge between Swiftcurrent and Boulder creeks as ‘Boulder Ridge.”’ The
ridge north of Swiftcurrent Creek will be referred to as “Swiftecurrent Ridge.’ The
name “Kennedy Ridge’ will be applied to the ridge with two crests north of North Fork
of Kennedy Creek.
690 w. cdc. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
TOPOGRAPHY OF THE PLAIN
The terminal moraine of the Keewatin ice-sheet was traced northward
across the Cut Bank quadrangle to the international boundary, in longi-
tude 112 degrees 20 minutes west, by Mr. Calhoun’ in 1902. From this
point the margin of the Keewatin drift trends westward, in part north
and in part south of the 49th parallel, to Waterton River. Going west-
ward from the terminal moraine across the Blackfeet Indian reservation,
one finds the area characterized by the topography which is delineated
on the Cut Bank, Blackfoot, and Browning topographic sheets, and
which has been described by Willis® and Calhoun. It is a great treeless
plain, in places nearly flat, but mostly rolling to hilly, rising gradually
toward .the mountains. Standing above the plain here and there in the
eastern half of the reservation are butte-like eminences or small elevated
plateaus and elongated ridges, with abrupt, incised marginal slopes.
These have reliefs of several hundred feet above the valley bottoms.
Farther west such elevated tracts gradually coalesce into broader pla-
teaus or larger ridges which are particularly characterized by smooth,
nearly flat surfaces. Approaching the mountain front, bulky ridges
stand at either side of the principal valleys heading in the range and
~ lead directly up to the bases of the bold salient mountains which guard
the portals to the park. Adjacent to the mountain front these ridges
attain elevations ranging from 5,900 to 6,400 feet above sealevel and
stand 800 to 1,600 feet above the intervening valley bottoms. ‘Taken
together, the flat-topped ridges and plateaus have the appearance of being
remnants of a continuous high-level plain which once sloped gradually
eastward from the base of the mountains, but which has been so reduced
by long-continued stream erosion that but a small part of the original
surface now remains.
Describing these features in his paper on the “Stratigraphy and struc-
ture of the Lewis and Livingston ranges,” Mr. Bailey Willis writes:
“The highest surfaces of the plains are limited in extent, constituting accord-
ing to field estimate not more than one-fiftieth of the total area. Nevertheless
their profiles fall into a uniform line that represents an ancient plain, due to
the erosion of the Cretaceous shales and sandstones of unequal hardness. The
extent and uniformity of the plain are very marked, and it is the initial
physiographic fact of the region. It is herewith designated the Blackfoot plain,
after the Indian tribe whose name is associated with the region. On this
ancient surface there is a widely distributed thin layer of gravel which is
supposed to antedate the Pleistocene deposits.”
SOp. cit, p. 22.
6 Bailey Willis: Stratigraphy and structure of the Lewis and Livingston ranges, Mon-
tana. Bull. Geol. Soc. America, vol, 13, 1902, p. 310.
‘74
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 38
Sraswa
FIGURE 1.—Two MEDICINE RIDGE OF UPTURNED AND BEVELED CRETACEOUS SANDSTONE
In this part capped with coarse ‘‘quartzite gravel’? and farther west with pre-Wiscon-
sin glacial drift. Moraine of Two Medicine glacier of Wisconsin stage in the foreground.
FIGURE 2.—PRE-WISCONSIN GLACIAL TILL, LARGELY CEMENTED TO TILLITE CONGLOMERATE
EXPOSED AT WEST END OF UPPER PART OF TWO MEDICINE RIDGE
PRE-WISCONSIN GLACIAL MATERIAL IN MONTANA
EE —
TOPOGRAPHY OF THE PLAIN 691
Inasmuch as the investigations of the past summer were confined
principally to observations in and adjacent to the mountains themselves,
a thorough examination was not made of all these elevated tracts on the
plain, and the deposits lying on them were not seen far from the moun-
tains. The results of the observations that were made, however, are so
significant that a preliminary statement. concerning them seems war-
ranted at this time.
Beginning at the south, a brief description will be presented of the
character and relations of the deposits on the several high ridges ex-
amined by Mr. Thomas and the writer in the belt near the mountains.
Deposits oN T'wo MeEpDICcINE RIDGE
Issuing from the mountains about 7 miles northwest of the village of
Midvale, Two Medicine River swings to the southeastward and traverses
the plain in a sharply cut, trenchlike valley. The lower lake lies about
800 feet below the level of the rolling drift-covered plain on the east.
Going northward from Midvale across this plain one finds well marked,
though mildly developed sag-and-swell morainal topography set with
numerous little ponds. This marks the marginal moraine of the Two
Medicine glacier of the Wisconsin stage (plate 39, figure 1). It ends
at the north along a fairly definite line near the foot of the south slope
. of a long flat-topped sandstone ridge, part of (plate 38, figure 1) “Two
Medicine Ridge.” ‘To the east the ice extended through the gap in the
sandstone ridge, which is traversed by the Great Northern Railroad and
spread over the lower land toward Browning. South of the railway the
glacier overtopped the ridge and left later glacial drift thereon. Through
a length of 314 miles northwest of the railway the ridge was not sur-
mounted by the later ice-sheet. That part of the ridge shown in plate
38, figure 1, has a relief of about 200 feet. Ascending the abrupt slope,
the top is found to be notably flat excepting where cut by a ravine which
partially divides the ridge. It rises gradually westward from 5,300 to
5,600 feet above the sea. This plateau surface, which is a remnant of
the Blackfoot peneplain, is beveled across the edges of the Cretaceous
sandstone, which at one point noted has a dip of 42 degrees toward the
southwest. Capping the ridge is a thin deposit consisting of gravel
ranging in size from fine to boulders 114 feet long. The stones are
partly well rounded, but mostly subangular. They are principally of
quartzite, white, yellowish, banded pink, and red, and with these are
pebbles of maroon argillite, green argillite, and diorite, named in the
order of relative abundance. All these rocks are from the pre-Cambrian
formations of the mountains to the west, and the same kinds of pebbles
692 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
and boulders comprise the coarse material of the later glacial drift on
the adjacent plain below. The only constituents of the later drift not
found on this part of the ridge were limestone and a quartzite con-
glomerate containing pebbles, of black chert, which occurs principally in
the drift somewhat farther south and is from ledges exposed in the pass
traversed by the railway and provisionally referred by Doctor Stanton to
the Lower Cretaceous. Fragments of this conglomerate may never have
been deposited on this upland tract, and the limestone if deposited may
have been removed by solution. Careful examination of the pebbles
failed to reveal any showing glacial striation.
Going westward, the undulating drift plain gradually rises, and north-
east of Lower T'wo Medicine Lake for about a mile the later drift over-
laps the higher plain. Crossing this interval, the sandstone ridge rises
above the later drift plain, increasing rapidly in height, until one stands
on a flat-topped mesa with an elevation of 6,200 feet above the sea, a
height of 400 feet above the margin of the later drift, a relief of about
1,350 feet above the lake. Here there is a somewhat thicker deposit of
the same material and among the pebbles a few of limestone were noted.
This high tract has a length of about half a mile. Beyond this there is a
sharp drop in the crest of 100 feet or more. West of this sag the crest
rises again until the 6,200-foot level is attained.
On the day following that on which this part of the ridge was exam-
ined, approaching the ridge from the northeast, we climbed 1,200 feet
from the South Fork of Cut Bank Creek, over slopes of upturned and
folded sandstone, till we reached the flat top of the western part of Two
Medicine Ridge. On this top were found coarse gravels and boulders of
the same character as noted farther east. Many of the stones, however,
were much larger, some being boulders 8 feet in length. The deposit
seems to thicken toward Two Medicine Valley, and at the southwest ex-
tremity of the half-mile-wide mesa top a fresh scarp, due to slumping of
the underlying Cretaceous, exposed 150 feet of the material. Here the
deposit is typical glacial till (figure 2, plate 38). There is no assort-
ment or stratification, the stones, which range in size from small pebbles
to boulders 8 feet in length, being heterogeneously mixed and imbedded
in a matrix of reddish clay. A large part of the deposit is cemented by
calcium carbonate to hard, tillite conglomerate. This stands with ver-
tical face and as towers 15 to 25 feet in height. Some of the stones are —
well rounded, but a large part of the pebbles and boulders are sub-
angular, facetted, and beautifully striated (figure 2, plate 39). The
material is wholly derived from the mountains, being of the same litho-
logic character as the gravels found on the ridge farther east. Lime-
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 39
FIGURE 1.—MORAINE OF THE TWO MEDICINE GLACIER OF THE WISCONSIN STAGE AT A
POINT 5 MILES NORTHEAST OF MIDVALE, MONTANA
FIGURE 2.—GLACIATED BOULDERS IN PRE-WISCONSIN GLACIAL TILL EXPOSED AT WEST
END OF Two MEDICINE RIDGE
PRE-WISCONSIN GLACIAL MATERIAL IN MONTANA
DEPOSITS ON TWO MEDICINE RIDGE 693
stones are rare among the stones scattered over the mesa top and also in
the upper part of the 150-foot section. Farther down the slope, how-
ever, they become more numerous and show less effects of weathering.
It is probable that the calcareous cement of the conglomerate was de-
rived from solution of the limestones in the upper part of the deposit.
This exposure faces the mountain slope at a distance of something over
a mile. Between the two the ridge has been lowered and narrowed by
erosion. This lower part is densely timbered and was not examined.
From this narrowed divide the valley between the high mesa and the
much higher mountain slope deepens rapidly northward to a level 1,000
feet below the top of the former. ‘The composition of the deposit, its
topographic situation relative to the mountains, to the present drainage
lines and to the deposits made by the glaciers of the Wisconsin stage, the
modification by weathering, and the cementation to a heavy bed of con-
glomerate all indicate that we have here a glacial deposit of relatively
great age. If all the dissection of the Blackfoot peneplain was accom-
plished in the interval between deposition of the high level and the low
level drifts, the earler glacial extension antedated the Wisconsin glacia-
tion by a very long time.
North of this drift-capped ridge are numerous much lower hills and
ridges of sandstone and shale. On one of those examined a few pebbles
of quartzite and diorite were found, but on the others there was no evi-
dence of this older drift. Among these hills flow tributaries of South
Fork of Cut Bank Creek. One of these, Lake Creek, heads in glacial
cirques in the mountains, and, stretching eastward on either side of the
valley, are the finely developed moraines of a glacier of the Wisconsin
stage.. At its greatest extension Lake Creek glacier had a length of
about 10 miles. At points equally distant from the mountain front the
crests of these moraines of Lake Creek glacier stand 500 feet lower than
the top of the high drift-capped mesa, and the bed of the stream between
them is 300 feet still lower.
Deposits on Cut Bank RIDGE
Between the South and North forks of Cut Bank Creek is a ridge of
Cretaceous shale whose crest 1 mile from the mountain front has an ele-
vation 6,300 feet above the sea. Standing on this crest one looks down
1,000 feet to the stream on the south and 1,200 feet to bottom of the
valley on the north. Both slopes are steep, that on the north being par-
ticularly precipitous, that on the south much less so. Shale is exposed
to within 100 feet of the top near the west end of the highest part of the
694 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
crest. Here there is an abrupt drop in the crest line, and from this point
~ to the mountain the crest is narrow, lower, and composed of shale. The
highest part of the ridge is capped with till and gravelly drift, which 1s
exposed at several points in fresh scarps due to landslides. The litho-
logical composition is the same as on Two Medicine Ridge and many of
the green argillite fragments show glacial striations. This rock is very
dense, fine grained, and so difficultly soluble as scarcely to be etched at
all even after very long exposure to the weather. Some of the limestone
blocks are 6 to 8 feet in length. The top of this ridge is broad, smooth,
and gently sloping. The north slope is heavily timbered and there has
been much slumping of the drift on the underlying shale, so that the ©
upper limit reached by the North Fork glacier during the later extension
of the ice has not been accurately determined. Judging from the condi-
tion on the opposite side of the valley, the surface of the later ice was at
least 200 feet below the top of this ridge.
Between 4 and 5 miles east of the mountain the crest drops 300 or 400
feet to a sag. Through this sag the ice of the North Fork glacier of the
Wisconsin stage appears to have extended nearly or quite to contact with
that of the South Fork glacier. Beyond the sag the crest rises again 200
to 300 feet, maintains its height for about a mile, and again drops to a
much lower level, over which the later ice spread morainal deposits.
Two miles farther southeast the ridge, here of sandstone, rises again
above the later drift and extends thence eastward with even, flat top, 2
miles to the point where it is cut by the post-glacial gorge of the South
Fork of Cut Bank Creek. East of this creek the ridge continues toward
Browning, but is still lower and was overridden by the later ice. Both
the isolated mesa-like parts of the ridge are capped with coarse gravel,
largely quartzite, evidently to be correlated with the drift farther west
and on Two Medicine Ridge, although here no till and no striated Bs
were observed.
DEposits oN Minx River Rivage
On the north side of the valley of North Fork of Cut Bank Creek is
another great ridge of Cretaceous shales and sandstones left from the
erosion of the Blackfoot peneplain. This is known as Milk River Ridge
from. the fact that tributaries of that stream head on its north slope.
Down the great trough between Milk River and Cut Bank ridges Cut
Bank glacier extended at the Wisconsin stage of glaciation, attaining a
length of 12 miles east of the mountain front. Climbing 1,600 feet from
the valley bottom to the point where Milk River Ridge joins the moun-
tain front, one finds the deposits much disturbed by landslides, but it
le i i ld
.
DEPOSITS ON MILK RIVER RIDGE 695
looks as though the ice emerging from the mountain valley extended this
high up on the slopes. Overtopping the proximal end of Milk River
Ridge, the glacier appears to have spilled across the crest, extending a
small lobe about 2 miles northeastward down the slope on the north.
Perhaps this was assisted somewhat by ice descending from a fine big
cirque in the east slope of the mountain. ‘Two well formed lateral mo-
raines are seen curving northward through the east side of a sag in the
erest of the ridge. Crossing this sag and climbing to the high flat top,
which here stands at an elevation of 6,100 feet above the sea, it appears
that the last ice just overtopped the north slope at the west end of this
part of the ridge and left there a small marginal ridge of drift. This
may be traced eastward about three-quarters of a mile on the top of the
ridge; it then drops down to a lower level and lies along the slope 100
feet or so below the top. On the high flat part of the top of the emi-
nence, beneath and beyond the little marginal ridge, is a deposit of
coarse gravelly drift yellowed with age and in which no limestone was
observed, although a massive bed of limestone is exposed in the moun-
tain slope to the west, and derived fragments are plentiful in the later
drift. It does, however, contain striated pebbles. The character and
relations of this deposit show that there is here another remnant of the
old high level drift. At the east end of this mesa an abrupt slope drops
down about 500 feet to a second sag in the crest 114 miles in width.
This broad sag in the crest afforded another spillway for Cut Bank
glacier, and through this a tongue of ice extended northward a distance
of 3 miles into the Milk River Basin, spreading out on the lower ground
_ as a lobe over 2 miles in width. This small lobe is designated the Milk
River glacier by Mr. Calhoun.’
Crossing this second sag and climbing about 350 feet up a steep slope
one reaches the top of the main part of Milk River Ridge. From the
high west end one looks out over an extensive and remarkably smooth
plateau, sloping toward the northeast. In the first 114 miles the surface
declines 300 feet; beyond this there is a fairly uniform slope of nearly
80 feet per mile for 514 miles, the farthest distance to which the tract
was traversed by the writer. Farther east deepening ravines cut the
plateau into digitate, flat-topped ridges, and these in turn give place to
successively lower separated buttes. This elevated plateau is the best
preserved and most typical remnant of Mr. Willis’s Blackfoot peneplain
seen by the writer.
The drift of the Wisconsin stage extends nearly to the top of the head
of the high level plain, reaching an elevation of 5,800 feet above the sea
TOp; cit, p; 20.
696 w.cC. ALDEN——-PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
and piling up in sharp knolls and ridges. This drift, however, overlaps
but little if any of the upper plain. Eastward from this point the
margin of the later drift gradually descends the eroded south slope until
in about 5 miles it hes 300 feet or more below the upland at the point
where the marginal moraine of the valley glacier swings off to the south-
ward across the valley plain.
Mr. Calhoun’ also determined that the ice, though nearly filling the
valley of the North Fork of Cut Bank Creek, “did not spread over the
plateau to the north.”
Underlying this extensive high level plain is a yellowish to brownish
oxidized gravelly deposit like that described above, consisting principally
of quartzite with much green and red argillite, diorite, and some lime-
stone. The stones are subangular to rounded, and it seemed to me there
was no notable decrease in size with increasing distance from the moun-
tains. Numerous boulders 1 to 114 feet in diameter are found 2 to 3
miles from the head of this plain and 8 to 10 miles from the mountains,
the source of all the material. That exposed in a ravine in the northeast
quarter of section 12, township 33 north, range 13 west, consisted of clay,
pebbles, and boulders mixed as in glacial till. In the southeast quarter
of this section 100 feet of unassorted material was found, and in the
northwest quarter of section 6, township 33 north, range 12 west, a
thickness of 150 feet was observed. Here and elsewhere glaciated peb-
bles were found, though these are nowhere abundant and consist mostly
of the green, quartzitic argillite. Such striated erratics were found in
the sides of the valley of Arnold Creek as far out on this plain as our
traverse was extended. i
It is the writer’s understanding that the deposit capping this Milk
River Ridge is included with what has been described as the “quartzite
gravels” and has been regarded as pre-glacial in time of deposition.
Where seen by the writer, however, this contains well striated pebbles
and has the general characteristics of glacial drift. It evidently should
be correlated with the deposit of Two Medicine Ridge as pre-Wisconsin
glacial drift.
Deposits oN SAINT Mary RIDGE
Emerging from the mountains between the bold salients known as
Divide Mountain and Singleshot Mountain, the waters of Saint Mary
River flow in a general direction nearly due north through the lower lake
and beyond until they cross the international boundary. Bordering the
8 Loc. cit.
DEPOSITS ON SAINT MARY RIDGE 697
lower lake and the lower part of the upper lake on the east is an undu-
lating tract about a mile in width composed of small hills and ridges of
shale mantled with drift and standing 100 to 300 feet above the lake
levels. From this a steep slope, most of which is heavily timbered, rises
to the crest of a broad ridge known as Saint Mary Ridge. The crest of
this ridge gradually lowers in elevation from south to north. It is
highest between 2 and 3 miles north of Divide Mountain, there standing
about 6,100 feet above sealevel. In the interval between this highest part
and the mountain there is a broad sag in the crest line where the top of
the ridge is 300 feet lower. Where highest the top of Saint Mary Ridge
stands over 1,600 feet above the level of the upper lake. From this high-
est part the northward decline carries the crest line down to a level
which, east of the foot of the lower lake, between 9 and 10 miles to the
northward, is about 1,100 feet above the water in this lake and 5,500 feet
above tidewater. Duck Lake hes in a big sag in the upland, so that the
crest of the ridge may be said to curve eastward on the south side of the
lake. The top of Saint Mary Ridge is broad and smooth.. From this
the plain slopes gradually to the eastward. Much of this surface has
been lowered by erosion by the headwaters of tributaries of Milk River,
but in the interstream areas the higher tracts still represent the Black-
foot peneplain.
Beyond the broad sag, in which hes Duck Lake, the Hudson Bay
divide continues as a broad high ridge similar to and really a part of
Saint Mary Ridge. This part of the ridge, which consists of Cretaceous
sandstones and shales, has not been examined. The ridge east of Saint
Mary Lake has not been thoroughly examined, but what was seen by Mr.
Thomas and the writer is significant in connection with this question of
pre-Wisconsin glaciation.
On the steep west slope of Saint Mary Ridge there has been consider-
able landsliding on the shale, which probably forms the bulk of the ridge.
At a few places near the top of the slope this slumping has produced
fresh scarps, giving excellent exposures of the material capping the ridge.
Following the trail southeastward from the foot of Upper Saint Mary
Lake for about 144 miles and then climbing the wooded slope, we
reached one of these scarps between 1,100 and 1,400 feet above the lake.
The exposure has a height of nearly 300 feet and a length of 500 feet or
more. The upper 30 to 50 feet (A) of the section is grayish glacial
till, in which the pebbles and boulders are of red and green argillite,
quartzite, gray siliceous limestone from the Siyeh formation, diorite, and
some buff limestone from the Altyn formation. It looks as though most
of the Altyn limestone pebbles had been removed by solution and frag-
698 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
ments of the Siyeh limestone are deeply etched. Beneath this is (B) a
10 to 15 foot band, where the till is oxidized to an orange or yellowish
tint. In this is more of the yellow oxidized limestone, some of the frag-
ments of which are thoroughly rotted. Underlying this zone and form-
ing the greater part of the section is (C) reddish till cemented by cal-
cium carbonate to a hard conglomerate which projects from the slope as
ledges. Most of the pebbles and boulders in this have fresh glaciated
surfaces, but some of the diorites are disintegrating; many of the buff
limestones are etched by solution and some have been removed, leaving
only a yellowish powder in the cavities. The reddish tint is due to the
large amount of red argillite. The calcium carbonate cement was prob-
ably derived by percolating waters from the solution of limestone frag-
ments in the upper part of the section. It is the projecting ledges of
conglomerate which give to the deposit, as seen from the valley below,
the appearance of stratification. Close examination reveals no assort-
ment of the material or bedding. No fragments of rock were noted
other than such as are derived from the mountains. About 250 feet of
drift was seen, but the base was not exposed. About half a mile farther
south a second similar exposure of this was examined. Here the yellow
band (B) was not so noticeable, but other evidences of weathering and
cementation are the same. Four miles north of this later scarp a third
exposure was examined by Mr. Thomas. He reports 250 feet of drift of
much the same composition as noted above. No limestone was noted at
the top, though blocks of Siyeh limestone were seen in the conglomerate,
which extends to within 5 or 10 feet of the grassed top.
From the material exposed at these several points it is apparent that
the capping of Saint Mary Ridge is a deposit of old drift identical in
character with the old drift on Two Medicine Ridge excepting for the
presence here of fragments of Siyeh limestone. Owing to the thick
woods and the large amount of landsliding on the southern half of the
steep slope, the upper limit reached by the Saint Mary glacier of the Wis-
consin stage could not be determined there. Farther north, about a mile
south of the point where the ridge is crossed by the Babb-Browning road,
a small but definite morainal ridge begins to be developed somewhat
below the crest of the smoothly curved top of the big ridge. This small _
drift ridge, which is evidently the lateral moraine of Saint Mary glacier,
was traversed about 3 miles and found to be strengthening toward the
north. South of Duck Lake this curves eastward with the crest of the
big ridge. This moraine carries plentiful blocks of limestone, but on
the smooth broad top to the east little else than quartzite pebbles were
noted. As determined from the sections described, these “quartzite
DEPOSITS ON BOULDER RIDGE 699
gravels” represent the insoluble weathered residuals at the top of the
older drift. Taking everything into consideration, it is clear that the
heavy drift forming the capping of Saint Mary Ridge can not be re-
ferred to the last Saint Mary glacier, although that ice-stream so far
filled the valley as to overtop the high slope of the ridge east of the
lower lake.
Deposits ON RIDGE WEST OF LOWER SAINT Mary LAKE
On the west side of Lower Saint Mary Lake a correlative, but some-
what smaller ridge of Cretaceous shale and sandstone les between the
lake on the east and Flattop Mountain and Boulder Creek Valley on the
west. The crest of the ridge is narrow and serrate, consisting of a row
of sharp hills extending north-south on the line between sections 16 and
17, township 35 north, range 14 west. These peaks stand 5,700 to 5,900
_ feet above sealevel, 1,200 to 1,400 feet above the lake, and 500 to 700
feet above Boulder Creek. There is no very good exposure, but the ma-
terial seen on the surfaces of the knobs is like that of the drift described
above. Mr. Campbell reported that he found tillite conglomerate on top
of one of the hills. It is probable that this is a remnant of the pre-
Wisconsin drift. The surface of the ridge surrounding the line of hills
is marked by low swells and sags, the result of later drift deposition or
of landsliding or a combination of both.
Drposits oN BouLDER RIDGE
On the crest of the Cretaceous ridge between Boulder and Swiftcur-
rent creeks is a heavy deposit of glacial till which appears to be 200 feet
or more in thickness. This is exposed in fresh scarps due to slumping
at two or three places at the tops of the north and south slopes. The
pebbles and boulders in the reddish till are of limestone, red and green
argillite, quartzite and diorite, and are well facetted and striated. Ledges
of tillite conglomerate due to cementation protrude from the drift slope,
but there is no notable evidence of weathering and limestone pebbles are
present nearly or quite to the top. The top of this highest part of
Boulder Ridge is notably flat, like the crest of Two Medicine Ridge, and
has a length of about 2 miles. In this length the elevation increases
southwestward toward the mountain from about 6,100 to 6,300 feet
above tidewater. It thus stands 600 to 800 feet above Boulder Creek on
the south and 1,400 to 1,600 feet above Sherburne Lakes in Swiftcurrent
Valley on the north. At the southwest end of this flat top a short sharp
ridge rises to an elevation of 6,400 feet above the sea. The rise does not
XLIX—BULL, GEOL, Soc, AM., VOL, 23, 1911
700 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
continue to the front of Point Mountain, but after reaching this high
altitude the crest drops abruptly to a notch 200 feet or more in depth,
beyond which it again rises to Point Mountain. This sharp, highest
part of the crest of Boulder Ridge consists of chipstone of limestone,
white quartzite, and red and green argillite, such as compose Point
Mountain. No fragments of diorite were noted. The material does not
look like glacial drift but like talus, and its character and relation leads
to the suggestion that here is the last remnant of a disintegrated salient
of Point Mountain, which at the time of the deposition of this high level
drift extended 114 miles farther to the northwestward than it does at
present. The material is from the pre-Cambrian formations, which in
the nearest part of Point Mountain lie at elevations more than 800 feet
higher than does this remnant. This relationship indicates either that
the pre-Cambrian rock of this remnant was let down from a higher ele-
vation by gradual slumping or washing away of the underlying Creta-
ceous shale, or that, owing to a slight anticlinal fold, it originally stood
lower at this point than it does in Point Mountain, 1144 miles away,
where the rock is now inclined upward in the direction of the remnant
in question. Owing to similarity in component material of the older
and younger drift and to the slumped and wooded condition of the
slopes, it is difficult to determine just how high on the flanks of Boulder
Ridge the ice of Boulder Creek and Swiftcurrent glaciers extended at
the Wisconsin stage of glaciation. It seems clear, however, that the
later ice did not overtop the ridge, and that the drift capping the crest
of the ridge is that of a much earlier stage of glaciation.
DEPOSITS ON SWIFTCURRENT RIDGE
The companion ridge to that just described stands between Swift-
current Valley on the south and South Fork of Kennedy Creek on the
north. A subordinate part of this ridge extends northward at right
angles to the main ridge from Swiftcurrent Valley and forms the divide
between Saint Mary Valley on the east and South Fork of Kennedy
Creek on the west. The subordinate ridge, which rises 650 to 850 feet
above the bottom of the valley on the east, appears to have been over-
topped by Saint Mary glacier of the Wisconsin stage, inasmuch as mo-
rainal deposits are found along its crest. The summit of the main
ridge, which trends in a general east-west direction, appears not to have
been overtopped by the later ice moving down the valleys of either Swift-
current Creek or South Fork of Kennedy Creek. For 214 miles the top
of this ridge is very even (plate 40, figure 1), with a width of 90 to 120
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 40
FiGurRE 1.—FLAT Top OF SWIFTCURRENT RIDGE, A REMNANT OF THE BLACKFOOT PENE-
PLAIN, CAPPED WITH PRE-WISCONSIN GLACIAL DRIFT
Looking northwestward to Yellow Mountain in background, Appekunny Mountain at
left, and Chief Mountain at right
FIGURE 2.—MBESA OF “KENNEDY GRAVEL,” PROBABLY PRE-WISCONSIN GLACIAL DriFrt, 5
MILES EAST OF CHIEF MOUNTAIN
(Photo by Bailey Willis)
PRE-WISCONSIN GLACIAL MATERIAL IN MONTANA
DEPOSITS ON SWIFTCURRENT RIDGE 701
rods. It gradually increases in elevation from about 5,800 feet above
sealevel at the east to 6,000 feet at the west, so that it stands about 1,150
to 1,250 feet above Swiftcurrent Creek on the south. From this top
steep slopes decline on either hand. At the top of the south slope is an
abrupt scarp due to landsliding. This has a height of 200 to 300 feet,
and below is an uneven slope marked by swells and sags and numerous
small lakelets. This slope resembles morainal topography, but is prob-
ably principally due to slumping of the drift over the soft Cretaceous
shale. Two hundred feet or more of glacial till is exposed in the clean
scarp faces at the top of the slope. This drift is of the same composi-
tion and appearance as that on the ridge across the valley to the south
excepting that here, in addition to the other ingredients, fragments of
Siyeh limestone and amygdaloidal trap rock are found. The latter is
present in the mountains at the head of Swiftcurrent Valley. Many of
the pebbles and boulders are beautifully striated. Blocks of the tillite
conglomerate were seen, but no ledges clearly in place. Part of the
diorite boulders are considerably weathered so as to be exfoliating shells
half an inch thick, and some of the limestones in the upper part. are
etched but not removed by solution. The drift on the whole looks fresh
and shows but little modification by weathering.
At the west end of the high tract just described the ridge narrows and
the crest is broken by a sag about 1144 miles in length. This part is
crossed by the boundary between the Blackfeet Indian reservation and
Glacier Park. Here the drift capping has been removed and Cretaceous
shale is exposed at intervals. Beyond this the crest again rises and a
narrow remnant of the old drift remains. This part of the ridge was
examined by Mr. Thomas, but not seen by the writer. Mr. Thomas
reports a notched flat crest rising from 6,100 to 6,200 feet above the sea,
and scarps giving good exposures of 200 feet of glacial drift like that
forming the top of the ridge farther east, with ledges of tillite con-
glomerate in place. On the surface boulders of diorite and amygdaloidal
trap are conspicuous, some being 4 to 6 feet in length. The drift was
observed in place to within a few hundred feet of the pre-Cambrian
Altyn limestone in the east end of Appekunny Mountain. West of a
notch there is an abrupt rise to a bench at 6,300 feet above the sea.
This is cut in solid limestone and extends for a short distance about the
north side of the point of the mountain. On this bench no drift was
found. The top of the drift stands nearly 1,500 feet above Swiftcurrent
Creek on the south and 800 feet above South Fork of Kennedy Creek
on the north. From the topographic relations and the presence of the
tillite conglomerate, there is little room for doubt that this high level
702 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
drift is to be correlated with the other deposits described as having been
laid down by ice during a pre-Wisconsin extension of the mountain
glaciers.
DEPOSITS ON KENNEDY RIDGE
North of North Fork of Kennedy Creek in the area east of Chief
Mountain is a hilly tract underlain by Cretaceous sandstones. A part
of this at least was covered by ice at the last stage of glaciation, but
little of it was examined during the past summer. Rising above the
general level of this tract, just north of Kennedy Creek, is a small,
abrupt, flat-topped mesa having an elevation 5,800 feet above tide and
900 feet above the stream on the south (figure 2, plate 40). This was
described by Mr. Willis in his paper on the Lewis and Livingston
Ranges® as “the typical occurrence of the Kennedy gravels.” ‘The slopes
of this mesa are abrupt scarps due to landslides, and in places these
scarp faces are bare of vegetation and give good exposures of the com-
ponent material, 100 feet or more in height. ‘This material is coarse
cobblestone gravel and small boulders. A large part of the stones are
subangular and facetted and some of it is well rounded. No evidence of
. assortment or bedding was noted and, to the writer, the aspect was rather
that of gravelly glacial drift than of stream gravels. Moreover, careful
search yielded numerous pebbles carrying striations which, if not due to
glaciation, are certainly identical in character with such as were pro-
duced by glaciation. The stones, which are wholly pre-Cambrian rock
from the mountains, consist principally of buff limestone and quartzitic
material from the Altyn formation, and with this is a subordinate
amount of red and green argillite. Striations were found only on pieces
of the greenish dense quartzitic argillite. The surfaces of other pebbles
had been sufficiently etched and roughened by weathering to remove
striations if such were present. The ridge stands so high and is so
narrow and so exposed on all sides that conditions particularly favor the
surficial modifications of the material by the various agencies of weath-
ering.
Mr. Willis reports'® that Mr. George I. Finlay, who examined the
deposit, did not find striated pebbles. Concerning their interpretation,
he writes as follows:
“The constituent materials, the forms of the boulders and pebbles, the
obscure stratification, the topographic form, and the position of the mesa, all
characterize this occurrence as a remnant of an alluvial cone of Kennedy
® Op. cit., pp. 328-330.
1¢@ Op. cit., pp. 328-330.
DEPOSITS ON KENNEDY RIDGE 703
Creek. No earlier record has been detected in the history of that stream.
Since that date, however, the valley has been cut down 900 feet, a glacial
epoch has intervened, and the channel has recently been re-excavated and sunk
deeper in the subterrane.
“Certain tabular drift surfaces between Swift Current and South Kennedy
creeks and on the northern slope of Yellow Mountain are probably not of the
Kennedy formation, but are outwash plains beyond moraines. Gravel mesas,
that are correlative with the Kennedy and may be included under the forma-
tion name, occur in Canada, one lying 6 to 8 miles north by west from Chief
Mountain and east of Belly River; another, a group of three hills, occurring
east of lower Waterton Lake, a few miles north of the boundary. The basis of
correlation in these two cases is general form, altitude, and constitution of the
masses, which were not, however, examined in detail.”
The character and relations of the deposit on the ridge between Swift-
eurrent and South Kennedy creeks have:already been described. ‘The
mesas in southern Alberta on the east sides of Belly River and Waterton
Lake were seen but were not examined. Neither was the tabular surface
on the slope of Yellow Mountain examined.
In discussing the relations of the Kennedy gravel mesa, Mr. Willis
refers to it as “isolated and equalled in height among the outlying hills
only by a ridge of Cretaceous sandstone about 100 feet higher and 2
miles west of it.” After examining the Kennedy gravel mesa, Mr.
Thomas and I crossed the intervening sag, which is nearly 300 feet in
depth, and ascended to the top of the south end of this Cretaceous ridge.
The smooth top of this eminence rises to an elevation 5,900 feet above
the sea, about 100 feet higher than the mesa to the east. On the west
the surface drops down between 300 and 400 feet to a sag in the divide
between Kennedy and Lees creeks, and beyond this sag the slope rises to
the foot of Chief Mountain about 214 miles away. At the point of the
ridge facing Chief Mountain, in northeast quarter of section 26, town-
ship 37 north, range 15 west, fresh scarps have been produced by sliding
on the underlying Cretaceous sandstone and shale. These show the cap-
ping of the ridge to be 100 feet or more of typical glacial till. This til!
is very stony, reddish below and gray above and very compact, probably
partially cemented. The pebbles and boulders, a large part of which are
finely facetted and striated, are mostly from the Altyn limestone, with
subordinate amounts of greenish argillite and some red argillite. The
till is notably fresh in appearance, but I attribute this fact to its having
been so recently exposed.
I do not know the height attained by the ice of the last iene
Creek glacier. It may have spilled northward through the sags on either
side of this ridge, but I doubt if the ridge was overtopped; certainly the
704 w.c. ALDEN——PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
gravel mesa to the east stood at least 200 feet above the limit of the later
ice. From its elevation and its isolated position it seems to me that the
drift capping of this ridge is to be correlated with that on the mesa to
the east as a remnant of the pre-Wisconsin glacial drift.
DEPOSITS IN THE VICINITY OF BELLY RIVER
Crossing the ridge between Chief Mountain and the main front of the
mountain on the west, we descend the slope of Belly River Valley by the
old Indian trail. At about 6,300 feet above sealevel we passed from the
talus-covered slope of Cretaceous shale out along the crest of a scarp
produced by landsliding. This exposure showed the flattened top of the
ridge, between elevations 6,000 and 6,300 feet above the sea—that is,
between 1,300 and 1,600 feet above Belly River—to be composed of
glacial drift. On the following day Mr. Thomas made a more careful
examination, and he described the deposit as glacial till and gravel,
composed principally of hmestone and quartzite from the Altyn forma-
tion, with subordinate amounts of red and green argillite, some Creta-
ceous sandstone, and a few clay ironstones. Much of the material is
glaciated, the argillites showing striations most frequently. On a point
nearer the mountain beside the new trail is an exposure of a similar
deposit at about the same elevation.
Crossing to the west side of the valley, we climbed the heavily wooded
slope. Between 5,750 and 5,950 feet above the sea, or between 1,000 and
1,200 feet above the valley bottom, we found a bare scarp face, the mar-
ginal slope of a shoulder standing out on the slope. The material ex-
posed in this scarp is glacial till. All the pre-Cambrian formations are
represented in the pebbles and boulders of this drift, limestones from
the Altyn and Siyeh formations of the adjacent mountains, red and white
quartzite, diorite, and amygdaloidal trap. Many of the argillite pebbles,
especially, are well striated. Numerous blocks of tillite conglomerate
were observed, but no ledges were seen projecting in place. Above the
scarp the bench rises westward to the base of the cliff of pre-Cambrian
rock, but with a slope much less steep than the general slope of the valley
wall below. A similar bench, but somewhat less well marked, occurs to
the north just across the ravine. No exposures were seen to show
whether or not this bench is on a deposit of till. Seen from the east
side of the bottom of the valley, the two appear to be parts of one bench,
cut through by a broad sag, in the bottom of which is a sharp V-shaped
ravine which drains two glacial cirques in the mountain slope above.
This relation, taken together with the form of the bench and the char-
“Se DEPOSITS IN VICINITY OF BELLY RIVER 705
acter of the underlying deposit, suggests that the drift composing the
bench was deposited under the same conditions as that capping the flat-
topped ridges and mesas at a pre-Wisconsin stage of glaciation; that
during the later extension of the Belly River glacier a tributary ice-
stream, heading in the cirques above, cut through the bench, forming
the broad sag, and that, after the melting of this glacier and that in the
valley, post-glacial drainage cut the sharp notch.
Going northward along the slope to a point about one-half mile south
of the international boundary, another similar bench is found at about
the same elevation, with an exposure in the steep marginal slope, showing
glacial till similar to that described above. The sides of the valley are
heavily wooded and no detailed examination of them was made, so that I
am not prepared to say what was the upper limit of the last glaciation,
but I doubt very much if it overlapped these high-level deposits. These
benches stand like remnants of high level terraces and appear to repre-
sent a former stage in the development of the valley.
Crossing the line into southern Alberta, high, straight-topped ridges
like those described above were seen, one on either side of Belly River
and one east of Lower Waterton Lake. Unfortunately, however, owing
to a heavy fall of rain and snow, we were unable to examine the tops of
these ridges. Seen with field glasses from the valley below, there ap-
peared to be a heavy capping of coarse gravel on the ridges bordering
Belly River, and since seeing the other high-level deposits I will be sur-
prised if there are not on these ridges remnants of the same pre-Wis-
consin glacial drift.
AGE oF THE HIGH-LEVEL DRIFT
Until further investigation of the relations of these deposits have beer
made no satisfactory conclusions can be drawn as to their full signifi-
cance. As stated above, these flat-topped tracts have been regarded as
remnants of a late Tertiary peneplain. If the widespread “quartzite
gravels” capping these elevated. tracts away from the mountains are to
be correlated with this older glacial drift, then we may infer that the
drift was deposited prior to the dissection of the Blackfoot peneplain,
since the gravels must have been deposited prior to such dissection. The
presence of glaciated pebbles in the deposit capping Milk River Ridge,
the most typical remnant of this Blackfoot peneplain, and their presence
also in the type exposure of the “Kennedy gravels” certainly point to
such a correlation. If the valleys between these high-level tracts have
been excavated to depths of 900 to 1,600 feet, and the headward ‘exten-
706 Ww.c. ALDEN—-PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
sions of these valleys into the mountains have been correspondingly
deepened since the deposition of this drift, we must refer a considerable
part of the sculpturing of the mountains to Pleistocene time, for the
contours marking the levels of the tops of this drift extend far up toward
the heads of the mountain valleys, in most cases nearly or quite to the
cliffs below the upper cirques.
Discussing the “Kennedy gravels,’ under the heading “Pleisto-
cene (?),” Mr. Willis? wrote in part as follows:
“Gravels are widely spread on the highest tables of the plains north of Cut-
bank River and between the forks of Milk River. Their position suggests a
correlation with the Kennedy formation. On the other hand, the gravels of
the plains are composed chiefly of quartzite and presumably have lost the more
soluble constituents, which still occur in the Kennedy formation. From this
distinction greater antiquity may be argued for the high-level gravels of the
plains. .
“Salisbury in summarizing the results of Calhoun’s investigations in 1901,
in this region, says :”
“The high-level quartzite gravels on the plains east of the mountains are
believed to be deposits made by streams at the close of the first epoch of base-
leveling recorded in the present topography.
“Tf this belief be confirmed, the high-level gravels of the plains and the
Kennedy formation are alike in genesis and derivation from the Lewis Range.
They may, nevertheless, belong to widely different stages of uplift and erosion.
The characteristics of the gravels and the physiographic record of the moun-
tains may decide the relation on closer study.”
Inasmuch as we have shown that both the gravels on Kennedy Ridge
and those on a considerable part of Milk River Ridge contain glaciated
material, the relation to the “quartzite gravels” farther east is probably
somewhat different from what Mr. Willis had in mind, yet it is possible
that they do belong to “widely different stages of uplift and erosion.”
A part of the “quartzite gravels” may be pre-glacial stream gravels, as
believed by Calhoun, and much of the dissection of the Blackfoot pene-
plain and the correlated deepening of the mountain valleys may have
been accomplished prior to the deposition of the high-level glacial drift.
Mr. Campbell has suggested that instead of issuing from the mountains
onto an undissected plain the earlier glaciers may have extended down
valleys already cut in the’ plain, though to less depth than at present,
and have spread laterally over the higher tracts on either side, leaving
the thick drift largely as lateral moraines from which outwash deposits
11 Op. cit., p. 329.
1™2R. D. Salisbury: Glacial work in the western mountains in 1901. Journal of Ge-
ology. vol. ix, November-December, 1901, p. 721, [Incorrectly cited by Mr, Willis as
from January, 1902, number of this journal.]
AGE OF THE HIGH-LEVEL DRIFT 707
spread, as over the broad plateau of Milk River Ridge. The thick de-
posits of drift adjacent to the valleys then acted as a protective capping,
preventing the lowering of the thickly covered tracts while uncovered or
less thickly covered adjacent tracts were further reduced. On this in-
terpretation the high-level drift would still be referred to a pre-Wiscon-
sin stage of glaciation, but the length of the succeeding interglacial
interval would not be so great and less of the sculpturing of the moun-
tains would be referred to Pleistocene time. Further investigations will
be required to learn the full significance of this high-level drift, includ-
ing its relation to the “quartzite gravels,” which Dawson and McConnell
found underlying the Keewatin drift in southern Alberta and Saskatche-
wan and grading westward into drift of the mountain glaciers, to which
Doctor Dawson gave the name “Albertan” drift.**
DISCUSSION
Mr. Presipent: In answer to Doctor Atwood’s question whether the
pre-Wisconsin drift was deposited by valley glaciers rather than an ice-
cap, | would say, in my opinion, it was deposited by valley glaciers, inas-
much as it is now found just east of the mountain front capping the
ridges closely adjacent to the main valleys heading in the mountains.
In these places the drift capping protected the soft Cretaceous rocks
from erosion. Beyond, on either hand, where the drift may have been
thin or absent the peneplain was reduced.
Answering the second question, the peneplain is pre-glacial. The
drift was laid on the truncated edges of the upturned Cretaceous beds.
The age of the drift is independent of the age of the peneplain excepting
that it can not be so old as the plain. The important question is as te
whether or not the dissection of the peneplain occurred prior or subse-
quent to the deposition of the drift. If subsequent to the deposition of
the drift, then the drift is much older than that of the Wisconsin, and
a considerable part of the sculpturing of the mountains must be referred
to Pleistocene time, inasmuch as the contours marking elevations of
these flat-topped ridges extend far up the valleys, in several instances to
the foot of the cliffs below the cirques in the heart of the range.
The flat-topped mesas vary several hundred feet in maximum eleva-
tion, and it is not certain that all mark the same stage of deposition.
More work is required before accurate differentiation can be made.
I have not had the opportunity yet to work out the relations of this old
drift to the widespread quartzite gravels which have been regarded as
18 Geo. M. Dawson and R. G. McConnell: “Glacial deposits of southwestern Alberta .in
the vicinity of the Rocky Mountains.”’ Bull. Geol. Soc. America, vol. 7, 1895, pp. 31-66,
-
708 w.c. ALDEN—PRE-WISCONSIN GLACIAL DRIFT IN MONTANA
preglacial. A part at least of them may be outwash correlated with this
old drift.
In regard to Professor Coleman’s statement concerning the three drift
sheets differentiated by Doctor Dawson, I am as yet uncertain as to the
relations of this pre-Wisconsin drift to that described by Doctor Dawson.
As I understood the statements in Doctor Dawson’s papers, his old drift
was traced up the valleys between the higher foothills, although scattered
boulders were found on the latter. Here the old drift lies thick on top
of the highest of the foothills.
BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA
VOL. 23, PP. 709-712, PL. 41. DECEMBER 4, 1912
MINGLING OF PLEISTOCENE FORMATIONS?
BY B. SHIMEK
(Presented before the Society December 29, 1911)
CONTENTS
Page
IE eter re Ste tS tes Win a cisco ace ave wee eancnseeeeede wks 709
CRS eRe eens wat he ees Se wc c.ce ci G:s o's aie ou be 0 vieje wae sou mae 709
STE ET CUTS peg ESS ES ek eS le RIAA ee he
28 ae SS Cn Oe ee co ie 710
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rR RAM en Tee a ele aha eos ww dilwie ab Swe wie Ware eee lee 710
EE ESN AUS aE REE RIS esa gn a unis te 710
ee MESERE URED DE oes Sates re kG Sco ss as c's ceca geeue 710
Pe EP OP CCE E ee ee ic Se cal ce Sue ee cae aneen s 420
eR TASTER IONE oo od a Sal Sic. dic « « Stain ale © os ww sce ow pee uvede 711
6S STE i SCS a 0: eles yan!
0 gs ES eee) gt’ (yee Le 712
oe Te Bola StS aie OSE ae 2 a rs 712
Re terete ate) oi Sin a cts ais wie biclergu hae wate deveckewser 712
INTRODUCTION
Among the difficulties which beset the student of Pleistocene deposits
in the field, none cause greater perplexity than the real or apparent
intermingling of strata or masses belonging to different portions of this
period. It thus sometimes appears as if masses of different drifts are
transposed or interglacial formations are out of place.
Previous Work
Such intermingling has already been noted, particularly in connection
with the Aftonian, at Afton Junction, and Thayer, Iowa, by Calvin,’
_and in western Iowa by Calvin? and the writer.‘
1 Manuscript received by the Secretary of the Society December 29, 1911.
2 Proceedings of the Davenport Academy of Sciences, vol. x, 1905, pp. 18-30.
% Bull. Geol. Soc. America, vol. 20, 1909, pp. 137-139. A
*Ibid., vol. 20, 1909, pp. 406-7; vol. 21, 1910, p. 1833; Iowa Geological Survey, vol.
xx, 1910, pp. 351-2, 355 and 371.
(709)
710 B. SHIMEK——MINGLING: OF PLEISTOCENE FORMATIONS
RECENT OBSERVATIONS
ILLUSTRATIONS OF MINGLING
During the past year two striking illustrations of such mingling were
observed by the writer, the one at Des Moines, -lowa, showing a transpo- —
sition of yellow and gray loesses and a mixing of fossiliferous gray loess
with Wisconsin drift, and the other at Sioux Falls, South Dakota, show-
ing fossiliferous silt apparently between two drifts.
THE DES MOINES SECTION
Location.—This section was exposed for a short time in the excavation
made for the heating plant of the East Des Moines High School. The
locality. hes near the border of. the Des. Moines lobe of the Wisconsin
drift sheet, and loess is here frequently found under Wisconsin till.®
In a portion of the'section under consideration, however, an unusual
mingling of Pleistocene materials was observed during a visit made by
the members of the staff of the Iowa Geological Survey, which was sub-
sequently more closely investigated by the writer.
The loesses—Throughout the region under consideration two loesses
appear in many places. The lower is the usual bluish gray post-Kansan
loess, which is here frequently fossiliferous, and the upper is the common
yellow later loess. |
The Wisconsin drift—In the same region the Wisconsin till presents
a common yellow phase, throughout which small boulders and pebbles
are irregularly scattered. In the section under consideration a thickness
of 10 to 15 feet is exposed.
Mingled loess and drift.—In the lower 6 to 8 feet of this section there
appear gray bands and irregular streaks and masses which can not be
distinguished from the gray post-Kansan fossiliferous loess, excepting
for the presence of occasional pebbles, and, moreover, in a portion of the
section a larger stratum of this gray material lies above yellow loess, thus
producing an apparent transposition of the loesses.
A careful study of the section on the north and west sides of the exca-
vation, however, revealed the cause of this unusual relation.
On the west side at the base the section (plate 41, figure 1) exposes
about 5 feet of yellow loess with few fossils (c, figure 1). Above this is
a stratum of gray loess 2 to 4 feet in thickness, with a few pebbles, and
scattered shells of terrestrial mollusks for the most part broken. The
remaining 10 to 12 feet of the section show Wisconsin drift, in the lower
>See also McGee and Call on the Loss and associated deposits of Des Moines. Amer-
ican Journal of Science, 3d ser., vol, xxiv, 1882, pp. 202-328.
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 41
\
FIGURE 1.—SeEctTIon at East DES MOINES HicuH ScHoo.u
a. Yellow loess; b. Gray loess mingled with Wisconsin pebbles; ¢. Wisconsin drift
FIGURE 2.—SECTION AT S1oux FALLS
a. Gray silt with broken shells; b. Kansan drift
SECTIONS SHOWING MINGLING OF PLEISTOCENE FORMATIONS
J
,
’
;
THE DES MOINES SECTION 711
half of which there are masses and layers of gray loess containing a few
broken fossil land shells.
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On the north side the yel-
low loess soon disappears, as
shown in figure 1 in the text,
but the mixed gray layer,
here distinctly folded, ex-
tends for about 50 feet to
the east.
In this portion of the sec-
tion the lower 6 to 8 feet of
the Wisconsin also contains
masses of fossiliferous gray
loess.
To the eastward, on the
north side, the section
5 shows a distinct stratum of
33 typical fossiliferous and ap-
Be parently undisturbed gray
mS loess, exposed for 50 feet to
Ba a depth of 2 to 3 feet.
os A study of the entire sec-
: z - tion, as shown in text figure
a 1, suggests that the Wiscon-
sin ice, moving in a south-
erly or southwesterly direc-
tion, somewhat as indicated
by the arrow, pushed the
mixed gray mass (b) from
its position above (d) and
deposited it above the yellow
loess (c¢), which was also
more or less disturbed, as
indicated by a lateral ex-
cavation westward, which
ge shows an irregular mass of
Es yellow loess lodged above
ES the mixed gray layer (0).
Bs THE SIOUX FALLS SECTION
a Location.— The Sioux
a8 Falls section here discussed
712 B. SHIMEK——MINGLING OF PLEISTOCENE FORMATIONS
is located on the west side of Dakota avenue, north of West Third street,
in Sioux Falls, South Dakota. It presents another example of inter-
stratification which is of interest in this connection.
Briefly, the section shows a mass of gray silt lying between a lower
stratum of Kansan drift, of which 7 to 8 feet are exposed, and an upper
stratum of the same drift thickening northward to 10 or 12 feet.
The Kansas drift (plate 41, figure 2, b).—Both drift strata present
the usual characteristics of the western Kansan. The heavy bluish joint
clay is very calcareous and contains scattered pebbles and boulders.
The silt (plate 41, figure 2, a).—The silt is gray, calcareous, occa-
sionally mingled with broken fresh-water mollusk shells of the pond
types. The mass is exposed for about 75 feet, and distinctly dips down-
ward toward the south. Its greatest thickness is 3 feet, and at the north
it appears as if crowded or folded. Smaller masses of the same silt occur
in the lower part of the upper drift stratum.
Another section, on McClellan street opposite Main avenue, shows the
folding and crowding much better. Here a mass of silt, 20 feet long and
4 to 5 feet deep, imbedded in and completely surrounded by Kansan drift,
shows, on its northern side, distinct evidence of pushing and folding.
The conclusion that these masses of fossiliferous silt are older than
the Kansan, and that they were brought to their present position by the
Kansan ice, is certainly warranted. The silt is evidently Aftonian.
CONCLUSION
If narrow vertical sections of the two exposures here discussed were
made they would appear somewhat as follows:
The Des Moines section, west side:
Wisconsin drift, 10 to 12 feet (with bands of gray loess).
Gray, fossiliferous loess, 2 to 4 feet.
Yellow loess, 5 feet.
A normal section should show these loesses reversed and the larger sec-
tion here shows how the reversal had taken place.
The Sioux Falls section:
Kansan drift, 10 to 12 feet.
Fossiliferous silt, 3 feet.
Kansan drift, 7 to 8 feet.
In this case it would be easy to jump to the conclusion that the silt is
interglacial, separating ‘two distinct drifts. The larger section shows
that the Kansan is continuous and that the silt is intraglacial.
Manifestly, in both cases such sections would not show the true rela-
tion, and both show the need of great care in drawing conclusions from
sections of limited lateral extent.
BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA
VOL. 23, PP. 713-718, PLS. 42-43 DECEMBER 14, 1912
TOYALANE AND LUCERO; THEIR STRUCTURE AND
GENETIC RELATIONS TO OTHER PLATEAU
PLAINS OF DESERTS *
BY CHARLES R. KEYES
(Presented by title December 30, 1911)
CONTENTS
Page
ih hetiures Of tne Plaleal PlAIN, . 0... 61 eee cece wc cescasasece 713
PRT PIAGET PlalI) soc ee bie ce eel epee we sce s weosecsuceres 714
Tete ha a). iw ki gee aine Seat oe alc kisle sds cececeeccnesaemes 715
PE TILT EO IOI ee at, cic» a's Uhcn.e a hd sin dec isc ove veececencceuneies « 416
Holic character of the POSIONAl GLOS VEmMCLIVILICS 62s. ect ec caceactcasus fa a
DOMINANT FEATURES OF THE PLATEAU PLAIN
On the arid plains of the Southwest the two most striking features of
the landscape are the lofty isolated desert ranges and the lower trun-
-eated hills which rise abruptly as walls above the general plains surface.
The first mentioned of these relief characters has long attracted wide
attention from travelers; the second, notwithstanding the fact that it is
fully as impressive as the first, has scarcely received any notice at all.
R. T. Hill alone seems to have given them special consideration and a
name. For these plains above plains, or plains within plains, the term
plateau plains appears to be a very appropriate title. At the present
time particular interest attaches to the plateau plains because of the fact
that they seem to furnish the most direct and convincing testimony we
have of the deflative nature of general erosion under conditions of
aridity.
In the dry regions plateau plains appear as even surfaces, more or less
well elevated above the general plains surface about. As broad, trun-
cated mounds they rise out of the vast expanse of level earth after the
1 Manuscript received by the Secretary of the Society March 25, 1912.
(713)
714 C. BR. KEYES—TOYALANE AND LUCERO
manner of bold-coast isles out of a glassy sea. Mesas, or “tables,” the
Spanish-speaking people aptly denominate them. The margin of a mesa
forms the brow of a precipitous escarpment, which is one of its most
characteristic features. Not infrequently the upper part of the escarp-
ment is a vertical wall 100, 200, or even 500 feet in height. Mesa de
Maya (armored mesa) and Llano Estacado (walled plain) are Spanish
descriptive terms referring especially to this feature. The talus-like .
slopes below are steep, and their meeting with the general plains surface
is sharp. |
Profile and proportion are mainly functions of the geologic substruc-
ture. Some plateau plains are so small in area and so high that they
stand boldly out of the general plain as conspicuous cones, or buttes.
The Camaleon and Wagon Mound in eastern New Mexico are illustra-
tions. Others, as the Enchanted Mesa and the Covero, in western New
Mexico, and the Sunset Tanks buttes in Arizona, are only a few acres in
these. to. the. great. Chupadera Mesa and Mesa Jumanes, which are a
dozen miles- across: and a score of miles in length, or the vast Mesa de
Maya, which extends along the northern border of New Mexico a hun-
dred miles, there is every size.
STRUCTURE OF THE PLATEAU PLAIN
The foundation of the plateau plain is generally some rock layer more
indurated than the rest of the section. Structurally it may be made up
of (1) remnants of former plains worn out on the beveled edges of folded —
strata, as in the cases of the Mesa Jumanes and the Chupadera Mesa;
(2) slightly inclined strata of hard limestone or sandstone, which usually
are intercalated in extensive beds of less resistant materials, as in the
Chaca Mesa and other platform plains of the great Mesa Verde region ;
(3) almost horizontally disposed hard beds, from which the soft super-
posed layers have been stripped, as the Toyalané, El Moro, and the Tu-
cumeari; (4) old lava-sheets, which cover soft shales and sandstones of
which the Mesa de Maya, Mesa del Datil, and Acoma Mesa are conspicu-
ous examples, and (5) surface-wash deposits, locally hardened through
the evaporation of soil moisture, leaving the lime salts near the surface of
the ground, well represented by the Galisteo Ceja south of Santa Fe.
Most flat-topped hills are now commonly ascribed to cireumdenudation |
effects on an upraised peneplain. All remnants of the old graded surface
are on the same general level. Throughout the arid region the plateau
plains which rise above the surface of the general plains level also appear
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 42
7
cS on ill ane 5 os
~~
ae MF,
FIGURE 1.—FISHER PEAK, COLORADO
A spur of the Mesa de Maya, distant 15 miles and 3,500 feet above the basal plain
FIGURE 2.—TOYALANE, A TYPICAL PLATEAU PLAIN; NEAR ZUNI PUEBLO, NEW MEXICO
ILLUSTRATIONS OF PLATEAU PLAINS
STRUCTURE OF THE PLATEAU PLAIN 715
to be the direct result of cireumdenudation ; but, as will be seen later on,
of a somewhat different kind. In marked contrast to the humid-land
effects the remnantal plains of the desert, whether their surfaces be on
stratum planes, beveled tables of flexed strata, lava-sheets, or cemented
regolith, are of quite different elevations, even in the same district. In
New Mexico, for example, these plains attain all altitudes above the gen-
eral plains surface, from a few feet in the instance of the very recently
formed Malagro malpais, in the Hueco bolson, northeast of El Paso, to
the broad Mesa de Maya, which is 3,500 feet above the general plains
surface and 9,000 feet above sealevel (plate 42, figure 1). The Sierra
del Datil, in western New Mexico, has a magnificent northward-facing
escarpment 1,000 feet high, and in sight of it is the Acoma Mesa, 500
feet above the plains floor.
TOYALANE
Toyalané is a conspicuous flat-topped mountain (plate 42, figure 2),
situated in the Zuni Basin just over the continental divide in western
New Mexico. The region is the largest, highest, and driest desert plain
in this country. For the most part it lies 7,000 feet above tide level.
Structurally and topographically it constitutes an essential section of the
great Colorado dome, arching regularly from the Rio Grande to the Rio
Colorado. Save in one place—the Zuni swell—its broad surface is un-
broken by tectonic features. The region is preeminentlly one of plateau
plains standing at all heights above the general plains surface. To the
significance of this particular feature chief attention is here directed.
Around the southern slope of the dome there is, as Gilbert observes,
one of the great lava tracts of the world, second in magnitude in our
country only to the great northwestern lava field and fifteen times as
large as the classical district of extinct volcanoes in central France.
Sweeping in a broad crescent, 250 miles long, with Mount Taylor on one
horn and the San Francisco Mountain on the other, the main body of
lava flows, superposed in countless numbers, covers an area half the size
of New York State. Beyond the borders of the crescent are numberless
cinder cones, coulées, and limited lava-sheets, which spread out over the
soft sedimentaries constituting the substructure of the plains in this part
of New Mexico. In Arizona the hard Carboniferous limestone is the
main surface rock, the shales once overlying it having been recently
stripped off. Other volcanic evidences are the denuded necks and dikes.
Lava-sheets form the foundation of many plateau plains.
Outside the limits of the lava fields the massive and more indurated
L—BULL, GEOL. Soc. AM., VOL, 28, 1911
716 CG. R. KEYES—TOYALANE AND LUCERO
beds which are included between the thick sections of weaker strata take
the place of the lava flows in the formation of the plateau plains.
LAvA FLowS OF THE REGION
In the region under consideration extravasation of lavas h&s gone on
at frequent intervals from the very beginning of Tertiary times almost,
it may be said, to within the memory of men still living. The older
trachytic and andesitic lava-sheets of the Mount Taylor district now
stand 1,000 feet above the country around, and on this mesa rests the old
voleanic cone itself, higher and more impressive than Vesuvius. To the
north of Mount Taylor there are abundant evidences of still earlier vol-
canic activities, as shown in the forest of volcanic necks of that area,
from which is swept almost every vestige of their cones and the plains on
which they stood. Cabazon, a huge volcanic pipe, stands 1,200 feet above
its base and is a landmark for 80 miles about.
Much younger, and 500 feet below the Mount Taylor plain, is Acoma
mesa, 30 miles long and 15 miles wide, capped by basalt. At its foot,
another 500 feet lower down, is a great basaltic flow, 50 miles long by 20
miles broad, covering the present plains surface. Even more recent are
the coulées from the Tintero, on the Mesa Redonda, west of Mount Tay-
lor, which finally enter the channel of the Rio San José at a point con-
siderably below the level of the great flow just mentioned.
There are, then, four distinct periods of volcanic extravasation, be-
tween the first and last of which more than 1,000 feet of strata were
removed from the entire region about. There are in the district many
other lava-sheets at other heights; but between the four especially noted
definite time relations are readily established.
On the continental divide the streams are their smallest. On a vast
plain so situated drainage features are necessarily insignificant. Rain-
fall is the scantiest. These three conditions combined with arid climate
give water action small opportunity to vigorously erode. On every hand
the country clearly shows it. It is equally manifest that notable leveling
and lowering has gone on at a rapid rate. Since the Mount Taylor and
Datil plains levels were flooded with lava, general removal of surface rock
has taken place to the extent of more than 1,000 feet, as already stated.
The extensive erosion is of a peculiar type. There is little of the sharp
incision of the plains surface such as normally characterizes stream
action, especially in a high-lying region having slopes of high gradients.
Erosion is of the broad-basin type—wide, flat-bottomed, even plains be-
tween abruptly upturned rims against resistant rock-masses. As the lava
BULL. GEOL. SOC. AM. VOL. 23, 1911, PL. 43
FIGURE 1.—LUCERO TYPE OF PLATEAU PLAIN
North rim of the Jornada del Muerto of Socorro County, New Mexico, distant 30 miles
FIGURE 2.—STRUCTURE OF ROCK-FLOOR IN THE GALISTEO BASIN NEAR LOS CBERRILLOS,
NEW MEXICO
LUCERO TYPE OF PLATEAU PLAIN AND ROCK-FLOOR STRUCTURE
LAVA FLOWS OF THE REGION 717
flows and coulées became-more and more numerous the separate basins
became divided and smaller, but general lowering of surface went on
without interruption. There can be no question but that the lava-capped
mesas at varying heights represent former levels of the general plains
surface.
The lavas manifestly flowed down the lowest lines of the plains, but as
removal of the weaker beds on either side took place each flow was soon
left as an elevation (plate 43, figure 1). A particularly instructive in-
stance is shown near the Zuni pueblo, where an old valley is shown in
section filled with basalt, being exposed in a mesa face several hundred
feet above the present floor of the plain. Still more interesting is the
_ eoulée from the Sierra Lucero, at the northernmost extremity of the
Mimbres range and 40 miles west of Magdalena. In this district the San
Augustine plains are some 60 miles long and from 15 to 30 miles wide.
A high rim completely surrounds them, giving them interior drainage.
The substructure is mainly soft Cretaceous sandstones. From a mid-
point on the south rim, not so very long ago, Lucero sent out a narrow
coulée to the northward a distance of 15 miles, until it reached the oppo-
site wall of the plains in the Sierra del Datil. Since that time the gen-
eral surface of the plains has been lowered 50 to 100 feet or more. A
small playa now occupies a part of the western division of these plains.
Most of the basin plains of this region have rock-floors (plate 43, fig-
ure 2). It would be impossible for these basins to be filled with the
debris from the rims as has been ascribed to the Great Basin region.
To the north of the lava-capped mesas, mesa country still prevails, but
the table tops are indurated layers, such as are seen in Toyalané and El
Moro. When gently tilted, typical cuesta topography appears.
Eotic CHARACTER OF THE REGIONAL EROSIVE ACTIVITIES
That this high, dry, almost waterless waste on the continental divide
should owe its landscape features chiefly to deflation seems to need little
argument in this place. In the case of a district with alternating hard
and soft strata, the Toyalané type of mesa might not always offer con-
clusive evidence in support of this contention. Against the lava flows of
diverse ages as of the Lucero type no such objections can be raised.
These summit plains of the continent are a region of continual high
wind and constant sand-storm. Nowhere else in the arid region of the
Southwest is wind-scour in active operation so advantageously viewed.
Nowhere else in this country are deflative effects and desert-leveling so
well displayed. Nowhere else in all the world is general lowering of a
718 C. R. KEYES—TOYALANE AND LUCERO
country by the winds so strikingly presented. Few places there are on
this continent where stream action as a general erosional power is so
manifestly utterly impotent.
In the existence of plateau plains in the desert at many different levels
throughout the broad belts of the less resistant rocks there appears to be-
furnished one of the strongest proofs of the eolic character of the re-
gional erosive activities, since in situations of this kind not only are rain-
fall and water action very deficient and wholly inadequate to produce the
relief effects presented without the time element be vastly and unreason-
ably prolonged, but conditions are such in many cases as absolutely to
preclude the intervention of stream work.
BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA
VOL. 28, PP. 719-747 — DECEMBER 17, 1912
ABSTRACTS OF PAPERS PRESENTED AT THE TWENTY-
FOURTH ANNUAL MEETING OF THE SOCIETY, BUT
NOT PUBLISHED IN FULL IN THE PRECEDING PAGES
OF THIS VOLUME, TOGETHER WITH DISCUSSIONS OF
PAPERS AS FAR AS PRESERVED.
K. O. Hovey, Secretary
CONTENTS
Page
New evidence on the Taconic question [abstract]; by Arthur Keith....... 720
Some features in the Grand Canyon of Colorado River [abstract]; by
DRE DENIER ets Mra Uti ere dice wks’ s's See wba awe vet ece ceed oaae es (21
Pre-Cambrian formations in South-central British Columbia [abstract] ; by
eet: AS Daly... oc. sco. cee ee a ee ee oe e te ae 721
Covey Hill revisited [discussion]; by J. W. Spencer............ccccecee 722
Geology of Steep Rock Lake [abstract] ; by Andrew C. Lawson... ...... 722
Fossils of lower limestone of Steep Rock series [abstract and discussion] ;
IRIE TERI Ved ACCU Stett a oPve Efe ls Ml a Sk! cas Gis 'b's are ce wae ela esis led eee wee bb ale 723
Origin of the sediments and coloring matter of the eastern Oklahoma red
Deas fapsuract and discussion]; by J. W. Beede........ 6... cc ce we sens 120
Mesozoic stratigraphy of Alaska [abstract]; by G. C. Martin............ 724
Dark scale of hardness [abstract]; by Alfred C. Lane.................. 725
Demonstration of relative refraction [abstract]; by Alfred C. Lane....... 725
Stratigraphic study of the Appalachian and Central States with reference
to the occurrence of oil and gas [abstract]; by George H. Ashley...... 725
Granularity limits in petrographic-microscopiec work [abstract]; by Fred
Rieter eee ee eres ot ss ce ee as Vue ew eunet pews una cae 726
Arkansas diamond-bearing peridotite area [abstract and discussion]; by
I INN Ber ete tee ac as n'e wie os a'wicle'e vin'e.e ee ep ewe uae pm a slee 726
Variation of the optic angle of gypsum with temperature [abstract]; by
Demet. IRTAUG rt cs wide es geks eon» RP ee a ey es Pee RE Bt 726
Paragenesis of the zeolites [abstract and discussion] ; by J. Volney Lewis.. 727
Occurrence of petroleum associated with faults and dikes [abstract]; by
ER TPE HURT eens id Peers wis se ck bare wee ep ed ew eb eee ewe wee 728
Color scheme for crystal models [abstract]; by George Halcott Chadwick. 728
New minerals from the favas of Brazil [abstract]; by Oliver Cummings
ST CaN tae as icda'd: fk ba cic:e sid ed bie Swale P winlee a eee aie eae 728
Resins in Paleozoic coals [abstract]; by David White...............008. 728
Onyx deposits in east Tennessee [abstract]; by C. H. Gordon............ 729
Suggestion for mineral nomenclature [abstract] ; by Henry S. Washington. 729
Glacial deposits of the continental type in Alaska [abstract and discus-
729
Pie nee: Carr ang. Lawrence Martin... cies wr view eed ween as ones
720 ABSTRACTS OF PAPERS
/
Page
Pre-Wisconsin Glacial drift in the region of Glacier Park, Montana [dis-
cussion]:; by: Willianr Cov Alem. 5 oc .0s sii sds eke oe wee ee 730
Some Glacial deposits east of Cody, Wyoming, and their relation to the
Pleistocene erosional history of the Rocky Mountain region [abstract
and -discussion] ; by William J. Sinclair: .. 0.3 2. .0.<. 2 «eee: aon eee 731
Evidence of three distinct Glacial epochs in the San Juan Mountains of
Colorado [abstract]; by Wallace W. Atwood and:Kirtley F. Mather..... 732
Glacial investigations in Minnesota in 1911 [abstract and discussion] ; by
Frank. D@V@TeEE. Soo. ex Soic a a eee 6 wise whom whe tae ie ote anu See eee oh a 732
Grooved and striated contact plane between the Nebraskan and Kansas
drifts. [abstract]; by J. Ernest Carman... /...5.....5....: nn 735
Nebraskan drift of the Little Sioux Valley in northwest Iowa [abstract
and discussion]: by J. Ernest Carman........-.-.::.-..-+-.0en eee 735
On the pre-Glacial Miami and Kentucky Rivers [abstract]; by N. M.
PONNOMAI. «6 oc08 Hk Rs hives ds wm Gea Eee BED oom eee ROSE Re Ine coe 736
Recent studies of the moraines of Ontario and western New York [dis-
cussion] ; by Krank B. Taylor. os) .icitiec le. Oe 2 ee 736
Closing phase of glaciation in New York [abstract and discussion]; by
Hy. Fairchild s och son 2c a che tat! Gee ee er ee ee 737
Loess a lithological term [abstract and discussion]; by B. Shimek........ 738
Gros Ventre slide [abstract]; by Eliot Blackwelder..................... 739
Cenozoic history of the Wind River Mountains, Wyoming [abstract]; by
L. G.. Westgate and EB. B. Branson. os... 8. ooe4 a. us Sa cen G2 739
Stability of the Atlantic Coast [abstract and discussion] ; by Douglas Wil-
SOD. DOWMSOM 6! 55< oss sais Sa o's, 5 Sral's BoE Se bale Site Rimte cae eye se ee 739
Some coastal marshes south of Cape Cod [abstract and discussion] ; ; by
Charles A, Davis igccii e a)nccices ices ara2s untae etalon a aie alc a ep ene ee 742
Criteria for the recognition of ancient delta deposits [discussion]; by
Joseph, Barrell’. oii. eka os Gh wavelet ctees spe a eeciie eee! oe on eet ee 743
Ancient delta deposits [abstract and discussion] ; by A. W. Grabau....... 7438
Mississippian delta in the northern New River district of Virginia [dis-
cussion] 3. by H.. Bu. Bramsos « © 26 were e beeen isi, @ wns Vee ms en 748
Structure of esker-fans experimentally studied [abstract]; by T. A.
PRAT DH 58 Se 0 nse deck wl Brac bed whe Sw ee Pe acig? eatcte eT IS ee an 746
Effect of rapid offshore deepening on lake shore deposits [abstract]; by
Rufus M. Bagg, Dri cscs wiscale wiehs ive vie icvelataw, e's acces te agi a ie ene 746
Structure of the Helderberg front [abstract and discussion] ; a As We
GERDA Us 05.0 cee bia oie a. acaile lan ba te em lurid ie eis hurls (ee ied sebsate) wen eatna age ee ae 746
Succession in age of the volcanoes of Hawaii [abstract] ; by T. A. Jaggar, Jr. T47
Bibliography of the Mammoth Cave [abstract] ; by Horace C. Hovey...... TAT
NEW EVIDENCE ON THE TACONIC QUESTION
BY ARTHUR KEITH
(Abstract)
The reasons were given for reopening the old controversy and for selecting
the north end of the Taconic Mountain as the crucial place. The principal
views regarding the rocks of the Taconic Mountains were briefly outlined and
NEW EVIDENCE ON THE TACONIC QUESTION 721
the geology of the region summed up. Five subdivisions of the Stockbridge
limestone around the north end of the Taconics were described and attention
was called to the extreme folding and metamorphism of the rocks. The slates
of the mountains are sharply outlined from the Stockbridge limestone and the
eontact follows a rude semicircle around the end of the mountains. The char-
acters of this plane of separation were discussed and the conclusion was
reached that they could only be due to faulting. The bearing of this conclu-
sion was briefly considered.
SOME FEATURES IN THE GRAND CANYON OF COLORADO RIVER
BY N. H. DARTON
(Abstract)
Several years ago the author measured sections at a number of points along
the Grand Canyon to determine the stratigraphy of the Arizona Plateau.
These sections were presented, and there was exhibited a colored preliminary
geologic map of the Vishnu, Bright Angel, and Shinumo quadrangles similar
to one now in the corridor of El Tovar Hotel at Grand Canyon.
PRE-CAMBRIAN FORMATIONS IN SOUTH-CENTRAL BRITISH COLUMBIA
BY REGINALD A. DALY
(Abstract)
A reconnaissance along the Canadian Pacific Railway line has established
the following conclusions: 1. Dawson’s “Nisconlith series” occurring in the
Selkirk Mountains is not Cambrian, but represents the northern continuation
of the “Beltian” (Belt terrane) rocks at the International Boundary. 2.
Dawson’s “Nisconlith series” of the Shuswap Lakes area (west of the Selkirks)
is an entirely different pre-Cambrian and pre-Beltian group of sediments,
which unconformably underlie the “Nisconlith series” of the Selkirk section.
3. The Adams Lake volcanic series conformably overlies the thick limestones
of the “Nisconlith series” in the Shuswap Lakes area and. is of pre-Beltian
age. 4. The “Shuswap series” of the Shuswap Lakes is not a distinct gneissic
group unconformably underlying the “Nisconlith series,” but is the facies of
the “Nisconlith series’ produced where that series was thermally metamor-
phosed by batholiths. 5. Though these pre-Cambrian rocks are typical crys-
talline schists, their metamorphism of the regional type was not due to dy-
namie action; it was “static”? metamorphism (Belastungsmetamorphismus of
Milch). 6. The pre-Cambrian rocks are much less deformed (upturned) than
the overlying Carboniferous or Triassic rocks, illustrating the small depth of
the earth-shell which underwent strong folding in post-Cambrian time. 7. The
petrography of this pre-Cambrian and pre-Beltian terrane strongly suggests
that it furnished the greater part of the elastic material of the Rocky Mountain
geosynclinal prism. (Beltian and Cambrian sediments. )
COVEY HILL REVISITED
BY J. W. SPENCER
Published as pages 471-476 of this volume.
t22 ABSTRACTS OF PAPERS
DISCUSSION
Prof. J. B. WoopwortH stated in brief that the pool and accumulation of
blocks in “the Gulf” at Covey had been interpreted by Gilbert, himself, and
others as evidence of a torrential flow of waters out of all proportion to the
existing stream. As for the altitude of the upper marine limit on the north
side of Covey Hill, he had revisited the field since the paper, “On the ancient
water-levels of the Hudson-Champlain Valleys,’ was published, in company
with Professor Fairchil”, and accepted the latter’s determination of the upper
marine limit. The eievations given in that report were based on an old and
inaccurate altitude of Covey Hill, and can not be relied upon.
Prof. H. L. Farrcuinp: Dr. Spencer’s present views are a great change
from those of the last twenty years, during which he has advocated the ma-
rine origin of all the glacial lake beaches, including the Iroquois. Now he
doubts the marine origin of the lowest series of close-set bars in the Cham-
plain-Saint Lawrence depression, and which clearly correlate with deposits
containing marine fossils, and which have for nearly a century been recog-
nized by all workers as oceanic. There can be no doubt of the marine origin
of the Covey Hill beaches. The deformation of the Iroquois plane clearly
proves that the Covey Hill bars were below sealevel at the close of the
Iroquois time. The absence of a great cataract cliff at the Covey Gulf is
due to the fact that the ice-sheet lay close against the west slope of the
Champlain Valley or the east slope of the Covey Hill promontory, and the
outflow of Iroquois waters at the gulf was held up at high level and produced
the extensive areas of bare rocks on the Mooers quadrangle, formerly de-
scribed by Professor Woodworth. The history of this locality will be given
and the features described in my paper, ‘‘Closing phase of glaciation in New
York,” to be delivered later in this meeting.
Dr. SPENCER replied: Points emphasized in my paper are: That Covey Hill
Gulf is due to postglacial local erosion and not to drainage of a glacial lake;
that the spillway over the hill was from a glacial lake other than the Iro-
quois, probably an older one; that I saw no evidence then of any of the
beaches being marine. In making the original surveys of lakes Warren,
Algonquin, and Iroquois, I had adopted the hypothesis that they were not of
glacial origin. At that time the phenomena of the spillways had not been
well investigated. Since my return to these researches.I have accepted gla-
cial dams on fuller evidence. For this change of hypothesis, or progress, my
friend, Professor Fairchild, would impale me. But my former argument in
favor of the marine origin of Lake Iroquois he has adopted in support of
Gilbert Gulf, of whose existence I have failed to find evidence.
GEOLOGY OF STEEP ROCK LAKE
BY ANDREW C. LAWSON
(Abstract)
The paper gave a brief historical summary of the geology of Steep Rock
Lake and an account of a visit to the lake during the summer of 1911. The
observations that were made confirm the conclusion of Smyth as to the exist-
ence of the Steep Rock series as a distinct member of the Archean and its
GEOLOGY OF STEEP ROCK LAKE zo
unconformable relation to a granite gneiss of the basement complex. The
conclusion is that the Steep Rock series was unconformably deposited upon
the Keewatin. The probable position of the Steep Rock series in the geo-
logical scale is given as beneath the Animikie, with a series of quartzites and
slates, which is called the Seine series, between the Animikie and the Steep
Rock series. The discovery was announced that the limestone which was
estimated by Smyth to be not less than 500 or more than 700 feet in thickness
is fossiliferous.
¢
. Pa
re
FOSSILS OF LOWER LIMESTONE OF STEEP ROCK SERIES
BY CHARLES D. WALCOTT
(Abstract)
Notes on a description of a new genus and two species of sponges found by
Dr. Andrew C. Lawson in the limestone of the Steep Rock series.
DISCUSSION
Prof. A. P. CoLeEMAN: It is extremely interesting to hear of the discovery
of distinct fossils in the Steep Rock series, which other geologists as well as
myself have believed to be Huronian. The limestones are very fresh looking,
but hitherto no well-defined fossils have been found in them. There are,
however, carbonaceous beds in the Huronian which have been thought to
imply life, even though fossils were not known.
ORIGIN OF THE SEDIMENTS AND COLORING MATTER OF THE EASTERN
OKLAHOMA RED BEDS
BY J. W. BEEDE
(Abstract)
Recent investigations seem to show that the sediments of the lower red beds
of Oklahoma were derived from the Arbuckle-Wichita Permian land-mass.
The conclusion is based on the amount of material removed and the geo-
graphic distribution of sediments bordering the mountains.
Coarse limestone conglomerates of great thickness and conglomerates of
crystalline rocks, both possibly of subaerial origin, dovetail into red beds.
Belts of sandstone have been found extending into the area of finer sedi-
ments farther away from the mountains, apparently indicating the location
of stream debouchures at the margin of the shoal sea. The extreme shallow-
ness of the water is clearly indicated in the structure of the beds.
The coloring matter is thought to have been derived from the solution of
the 7,000 or 10,000 feet of pre-Carboniferous limestone which formerly coy-
ered the Arbuckle-Wichita Mountains and much of the surrounding region.
The solution of the limestone furnished optimum conditions for the oxidation
of its iron content, as it does at the present time in the limestone regions of
the Mississippi Valley, southern Europe, West Indies, and elsewhere. More-
over, the solution of the pre-Carboniferous limestones and the conglomerates
of the Arbuckle-Wichita region now in progress produces a red residuum
724 | ABSTRACTS OF PAPERS
practically indistinguishable from red beds sediments. The red granites, red
porphyries, and other crystalline rocks of the region under discussion con-
tributed their share of material to the red beds. Other factors may have
entered largely into the formation of the red beds of western Oklahoma.
DISCUSSION
Dr. I. C. Wuite: In the Monongahela series of West Virginia we get the
same kind of transition from fresh-water limestones to red shales in passing
from the northern portion of the State southwestward toward the Great
Kanawha River. There are no red beds whatever in the Monongahela series
at the northern line of West Virginia, but as the limestones disappear south-
westward red shales make their appearance, along with much more sandy
material in the shape of gray and brown sandstones.
MESOZOIC STRATIGRAPHY OF ALASKA
BY G. C. MARTIN
(Abstract)
Mesozoie strata cover vast areas in Alaska and constitute a large propor-
tion of the thickness of the local stratigraphic column. The recent work of
the U. S. Geological Survey has resulted in the accumulation of a great
amount of stratigraphic information which is chiefly either unpublished or
seattered through reports on local districts or on mineral resources.
This information is of importance not only because it constitutes so large
a proportion of the local geologic facts, but because there are obvious rela-
tionships in the Alaskan sections which contribute to a better understanding
of horizons in other parts of North America.
An attempt is made in this paper to summarize all existing information ;
to correlate the recognized horizons, not only between different parts of the
territory, but with the standard sections in other parts of the world, and to
present a proposed local classification of the Mesozoic rocks.
Triassic rocks are widely distributed in Alaska, and include over 5,000 feet
of marine sediments containing invertebrate faunas which permit of corre-
lation with several well-recognized horizons of the western part of the United
States and of Europe. Probably an equal thickness of voleanie rocks is
present.
The Jurassic is well developed throughout much of southern Alaska, and is
also present in the Arctic region. The Jurassic rocks are richly fossiliferous,
both marine invertebrate and plants being present. These faunas and floras,
although still largely undescribed, permit of correlation with the standard
European sections. Lower, Middle, and Upper Jurassic horizons are recog-
nized, the aggregate thickness of the fossiliferous Jurassic rocks exceeding
10,000 feet.
Both Lower and Upper Cretaceous rocks have been recognized in all of the
larger geographic subdivisions of the territory, the aggregate thickness of the
beds being many thousand feet. The Lower Cretaceous rocks are chiefly
marine and contain faunas allied to those of Russia. The Upper Cretaceous
rocks include fossiliferous marine sediments in which the Indo-Pacifie fauna
DARK SCALE OF HARDNESS 725
has been recognized and coal-bearing deposits of terrestrial origin. The lat-
ter possibly include beds transitional into the Tertiary.
DARK SCALE OF HARDNESS
BY ALFRED C. LANE
(Abstract)
The hardness of a mineral is its resistance to shearing stress. Like other
properties of minerals, it may differ in different directions. When two similar
surfaces are rubbed together, the softer mineral leaves a powder (streak) on
the other. In order to be sure which mineral gives the streak, it is at times
convenient to have besides the common Mohs scale of hardness, composed of
light minerals, a ‘dark scale of hardness” of minerals whose color and streak
are dark, especially in teaching. For such minerals the following properties
are desirable: quickly recognizable, easily obtainable, hardness uniform.
The following minerals have been used by the writer: (1) Graphite, with
one good cleavage, at one extreme in the white scale; at the other extreme in
the black. (2) Stibnite (Sb.S,), with two good cleavages, bladed. (3) Galen-
ite (PbS,;), with three good cleavages. (4) Iron (use soft wire nail), mag-
netic, ductile. (5) Niccolite (NiAs), characteristic color, no cleavage. (6)
Magnetite (Fe,0,), magnetic, brittle.
The minerals mentioned seem fairly satisfactory. Above 6 the author does
’ not know whether spinel or some other mineral would be more desirable, but
as there are comparatively few minerals concerned, it is not important.
DEMONSTRATION OF RELATIVE REFRACTION
BY ALFRED C. LANE
(Abstract)
The method of determining relative index of refraction developed by Exner,
Becker, and Schroeder van der Kolk* may be demonstrated to a class as fol-
lows: A large beaker of water placed just a little to one side of a window or
_other source of light will show a bright streak on the farther side, having a
higher index than the surrounding medium. A test tube full of air placed in
the beaker will show a bright streak of total reflection on the nearer side,
the air within having a less index than the surrounding medium.
STRATIGRAPHIC STUDY OF THE APPALACHIAN AND CENTRAL STATES WITH
REFERENOE TO THE OCCURRENCE OF OIL AND GAS
BY GEO. H. ASHLEY
(Abstract)
It had always been supposed by the oil and gas men that the Appalachian
region, extending from Pennsylvania to Alabama, was a stratigraphic unit,
and it has been a mystery that eastern Kentucky, Tennessee, and Alabama
should not yield as much oil and gas as Pennsylvania or West Virginia. The
1 Report Michigan Geological Survey, vol. vi, p. 154.
726 ABSTRACTS OF PAPERS
mystery largely disappears when a comparative study is made of the stratig-
raphy of the Appalachians as a whole. The paper compares graphically the
stratigraphy of the southern and northern Appalachians and the Central
States with reference to the occurrence of oil and gas.
GRANULARITY LIMITS IN PETROGRAPHIC-MICROSCOPIC WORK
BY FRED E. WRIGHT
(Abstract)
In this paper the petrographic microscope is treated as a measuring device
for the exact determination of the optical properties of crystal plates, espe-
cially of minute crystal fragments and of crystallites. The methods now
available for the purpose are considered briefly with special reference to their
accuracy and applicability to the investigation of fine-grained silicate prepa-
rations. Attention is directed in particular to the lower granularity limits at
which satisfactory measurements of the different optical properties of a min-
eral grain can still be made.
ARKANSAS DIAMOND-BEARING PERIDOTITE AREA
BY L. C. GLENN
(Abstract)
Evidence was offered of the circulation of presumably thermal waters about
the margin of the original pipe described by Branner. A supposed extension
of the peridotite area proves to consist of disintegrated peridotite mixed inti-
mately with well-rounded quartz sand and occasional water-worn chert peb-
bles and was evidently water-laid. Indications of the age of this material
narrow down the period within which the extrusion of the peridotite must
have occurred.
DISCUSSION
Prof. A. H. Purpure: The paper by Professor Glenn is of great interest to
me, for it appears to establish the age of the peridotites as post-Lower Cre-
taceous and pre-Upper Cretaceous, for recent work over the area by Mr.
H. D. Miser and myself had disclosed a marked unconformity in the imme-
diate locality of the peridotite, between the Lower and Upper Cretaceous.
The material of the intermediate area described by Professor Glenn was in
all probability put down while the Upper Cretaceous shoreline occupied this
area, the material, of course, having been derived from the disintegration of
the peridotite.
VARIATION OF THE OPTIC ANGLE OF GYPSUM WITH TEMPERATURE
BY EDWARD H. KRAUS
(Abstract)
By using an oil bath to determine the variation of the angle of the optic
axes of gypsum at different temperatures, it is found that gypsum is optically
uniaxial at approximately 90 degrees Centigrade for sodium light. Although
PARAGENESIS OF THE ZEOLITES Tae
Mitscherlich observed in 1826 that this change takes place at about 92 degrees,
the values given later by Des Cloizeaux, and more recently by Tutton, both
of whom used air baths, are from 15 to 26 degrees too high. Nevertheless,
Des Cloizeaux’s value of 116 degrees Centigrade for red light is the one com-
monly quoted. By plotting the values of the apparent angles of the optic
axes at various temperatures up to 132.5 degrees Centigrade, it is easily seen
that the angle changes most rapidly in the vicinity of the uniaxial point,
that is, between 80 and 100 degrees, and, further, that one axis, as was pointed
out by Naumann, changes its position more rapidly than the other.
PARAGENESIS OF THE ZEOLITES
BY J. VOLNEY LEWIS
(Abstract)
Zeolites and other secondary minerals occur in the Newark igneous rocks
of New Jersey. (1) Im cavernous spaces in the ropy pahoehoe of the extru-
sive Watchung basalts; (2) in fault fissures and fault-breccia of both the
basalts and the great intrusive sill (Palisades, Rocky Hill, and Sourland
Mountain) ; (3) less commonly in the ordinary joint cracks of both the extru-
sive and the intrusive types. The rocks are essentially the same in both
chemical and mineral composition, consisting essentially of pyroxene and
plagioclase feldspars, with quartz-bearing and olivine-bearing facies. The
zeolites and related silicates are essentially combinations of the feldspathic
elements and water, with the addition of fluorine in apophyllite and boron in
datolite; the accompanying amphibole, biotite, chlorite, epidote, serpentine,
and tale are derivatives of the pyroxenes. Hypotheses of origin dependent
on the action of meteoric waters are inapplicable on account of difficulties of
circulation, deoxygenation, and sources of fluorine and boron; on the other
hand, contact metamorphism by the intrusives has produced in the adjacent
shales minerals into which fluorine and boron enter, presumably by emana-
tion from the magma. Hence magmatic waters are regarded as the most
probable agent in the formation of the zeolites and accompanying minerals.
DISCUSSION
Prof. A. C. LANE: My experience would rank epidote somewhat higher.
Can we not conceive meteoric water working down, growing hotter, dissolving
silica, and becoming deoxidized by the reducing action of the basaltic glass
containing silica chlorides and hydrocarbons suggested by Brun, and thus
being in condition to deposit zeolites?
Prof. F. R. Van Horn: Professor Lewis spoke of apatite as evidence of
deep-seated waters being the cause of foundation of zeolites. I would like
to ask if he has been able to distinguish apatite of two origins—one by mag-
matic differentiation and another which is associated directly with zeolite
minerals.
Dr. Lewis replied: Apatite has been observed as a rock constituent, but
not seen in the vein minerals. It is possible to conceive of meteoric waters
penetrating the rock, becoming hotter with depth, and becoming charged with
the volatile magmatic emanations to such an extent that they would be prac-
tically indistinguishable from magmatic waters,
728 ABSTRACTS OF PAPERS
OCCURRENCE OF PETROLEUM ASSOCIATED WITH FAULTS AND DIKES
BY FREDERICK G. CLAPP
(Abstract)
Several instances of the occurrence of petroleum along faults and dikes
were described geologically and with reference to their place in the classifica-
tion of oil and gas accumulations.
COLOR SCHEME FOR CRYSTAL MODELS
BY GEORGE HALCOTT CHADWICK
(Abstract)
The proposed scheme of coloring uses the primary colors for the different
axes and applies to the various faces colors determined by the axis or axes
which the face parallels, with such modifications as are necessary, especially
in the isometric forms. The way in which this plan works out for the pyra-
mids and prisms of the tetragonal and hexagonal systems suggests a query as
to whether the ordinarily accepted usage of the terms “first order” and “sec-
ond order” in the hexagonal system is not exactly the opposite of their eco
eation in the tetragonal and possibly in need of rectification.
NEW MINERALS FROM THE FAVAS OF BRAZIL
BY OLIVER CUMMINGS FARRINGTON
(Abstract)
Study of the Favas accompanying the diamonds of Brazil (analyses by
H. W. Nichols) shows the presence of two new minerals. One, geraesite, is a
hydrous barium aluminum phosphate more acidic than gorceixite; the other,
minasite, is a hydrous aluminum oxide, which fills a gap in the series of
hydrous aluminum oxides and shows important parallelisms between the
hydrous oxides of iron and aluminum.
RESINS IN PALEOZOIC COALS
BY DAVID WHITE
(Abstract)
Resins are present in most coals, except possibly those of the highest
grades, the amount depending in general on the degree of concentration
(residual) resulting from the decay and reduction of the attending plant
structures. Interesting examples of megascopic resins in coals from the Car-
boniferous of the Mississippi Valley and Montana indicate the presence of resin
in the Paleozoic coals in proportions probably as large as in the coals of the
Mesozoic and Tertiary.
ONYX DEPOSITS IN EAST TENNESSEE 729
ONYX DEPOSITS IN EAST TENNESSEE
BY ©. H. GORDON
(Abstract)
The existence of onyx deposits in east Tennessee has been known for a long
time, and attempts have been made at recurrent intervals to utilize the ma-
terial. Thus far no success has attended these efforts, but with persistent
frequency hopes are aroused over some new “find” and glowing announce-
ments are made of the possibilities of this industry. The onyx found is of
eave formation and for the most part represents the remnants of vanished
eaves. The character and extent of the deposits and the possibilities of their
commercial development were discussed.
SUGGESTION FOR MINERAL NOMENCLATURE
BY HENRY S. WASHINGTON
(Abstract)
The science of mineralogy is a branch of descriptive chemistry, but in its
classification differs from it in that the crystal form is as necessary as the
chemical composition for the definition of a mineral. The nomenclature is
far behind the classification, and by its general use of a single termination
and arbitrary name roots gives no idea of the characters or relationships of
minerals. It is suggested that minerals be regarded as salts of mineral acids,
the salts being characterized by certain crystal forms, as was first suggested
by Penfield in discussing tourmaline and amphibole. The proposed names
will be formed in analogy with those of inorganic salts, the basic portion
being denoted by the chemical names of the base or bases, and the acidic
(negative) by adjectives ending in -ate for salts of sulpho- and oxy-acids,
and in -ide for binary compounds (sulphides, oxides), the root of this portion
being derived from the present name of some well known member of the
group, and the root implying always a definite crystal system and adherence
to a given type of chemical composition.
GLACIAL DEPOSITS OF THE CONTINENTAL TYPE IN ALASKA
BY R. S. TARR AND LAWRENCE MARTIN
(Abstract)
The. glaciation of the interior of Alaska forms a striking contrast with the
coast, where glacial erosion forms predominate, the deposits being largely
under water, except for (1) 1,600 square miles east of Yakutat Bay, (2)
16,000 square miles in the Cook Inlet-Susitna Valley region, and smaller
areas. The interior, between the Coast ranges and the Endicott-Rocky Moun-
tain system, where the National Geographic Society’s party made some studies
in 1911, has extensive glacial deposits of the continental type, previously
described in part by Russell, Brooks, and others, and similar to those of
United States. These include at least (@) 15,000 square miles in the Copper
River basin, (0) 27,000 square miles in the Tanana and Kuskokwim valleys,
730 ABSTRACTS OF PAPERS
(c) 17,000 square miles in the Yukon flats, (d) several thousand square
miles on the upper Yukon region in Canada and smaller areas. The domi-
nant material is outwash, and this extends long distances outside the country
actually glaciated. In places there is wind-blown loess associated with this.
In some localities it is still being deposited, and in the Copper River basin
it has been accumulating during the time required for the growth of six or
seven generations of trees. There is also some till, but this is largely buried
beneath outwash. Lake deposits, eskers, kames, and buried vegetation are
also found, but thus far no one has found drumlins. In thickness some of
these deposits rival those of the Middle West, one instance being known of
probably 800 feet of gravel, sand, etcetera, grading out from the mountains to
less than 100 feet fifty miles away. The presence or absence of these drift de-
posits seems to be chiefiy a matter of favorable topography and existing de-
glaciation—a process much like that formerly in progress in northeastern and
central United States.
DISCUSSION
Dr. C. A. Davis: The estimate of the age of the deposits shown in the
photographs, based on the age of the included stumps alone, is very conserva-
tive, since the stumps shown are thoroughly decayed. Such decay is usually
subaerial, and when once the stump is buried it practically ceases. If the
average age of the stumps shown in the strata were 150 years, 50 years
would probably be a fair estimate of the added time required to bury it
completely, so that at least 200 years is represented in each layer of stumps.
Prof. W. M. Davis called attention to the large volume of peripheral de-
posits as indicating large erosion in mountain sources of glaciers; still larger
when it is recognized that much glacially eroded material is not recognizable
in glacial deposits, but is washed far down the outflowing rivers and even to
the sea.
PRE-WISCONSIN GLACIAL DRIFT IN THE REGION OF GLACIER PARK,
MONTANA
BY WILLIAM C. ALDEN
Published as pages 687-708 of this volume.
DISCUSSION
Prof. A. P. CoLemMan: At Calgary, 100 miles north of the region spoken of
by Mr. Alden, there are two or three sheets of boulder clay. One coming
from the mountains is lowest and is covered by interglacial material, followed
by a boulder clay containing Laurentian boulders which came from the Kee-
watin center. The lowest boulder clay must be much older than the Wisconsin
ice age.
Prof. W. W. Atwoop: Mr. Alden has been working in a region of unusual
interest from the standpoint of glacial geology. It is probable that he will
secure some other significant data. I should like to ask a few questions.
Is it not possible that the Blackfoot peneplain, as described by Mr. Willis,
PRE-WISCONSIN GLACIAL DRIFT OF GLACIER PARK 731
exists in the area east of the mountains, but farther from the base of the
range than Mr. Alden has yet worked?
May not the Blackfoot peneplain pass under the older glacial drift, as
described by Mr. Alden?
Are the older glacial deposits described in this paper on the highest mesas
bordering the range, or are there still higher levels where there may be gravel
deposits, sometimes referred to as “high-level gravels?”
Are the older glacial deposits associated with the modern canyon in such a
way as to indicate that the ice which left them moved down these troughs?
SOME GLACIAL DEPOSITS EAST OF CODY, WYOMING, AND THEIR RELATION
TO THE PLEISTOCENE EROSIONAL HISTORY OF THE ROCKY MOUNTAIN
REGION
BY WM. J. SINCLAIR
(Abstract)
Twelve miles east of Cody, Wyoming, in the Eocene Bad Lands in the vicin-
ity of McCulloch Peak, angular blocks of Paleozoic limestone occur at eleva-
tions of 6,000 feet above sea, either on the crests of narrow ridges separating
deep valleys cut in the Bad Land clays or on terraces several hundred feet
above the Shoshone River. No other rocks than limestone have been seen in
these high-level deposits, but at lower levels abundant pebbles and boulders
of andesite may be found, all of which are water-worn, while the high-level
material is highly angular, the only sign of abrasion being the pitted surface
produced by the solvent action of rain water. Corals and bryozoa frequently
appear in relief on the rain-etched surfaces. Individual fragments vary in
‘size from a few inches or less to blocks 6 by S by 4 or 5 feet. The source of
the limestone is, undoubtedly, the Paleozoic formations of the mountains to the
west of Cody. Glacial ice is the only known agent capable of transporting
blocks of the size indicated. If they have been transported by ice, 1,200 feet
or more of canyon cutting has intervened since their deposition, for they are
stranded on narrow divides and comb ridges at least that high above the
Shoshone River. If they are to be correlated with the first glacial advance
in the Rocky Mountain region, much of the deep dissection of such inter-
montane troughs as the Bighorn Basin must be regarded as an event of
Pleistocene time.
Prof. W. W. Atwoop: It appears from Mr. Sinclair’s presentation that he
has secured some very important evidence on the recent physiographic his-
tory of the Rocky Mountains of Wyoming. I should like to ask him two °-
questions: How far away from the range are the large boulders which he
attributes to glacial origin? Are the deposits which he describes opposite
the present canyon in the mountains to the west?
Dr. Srncrair, in reply to the foregoing and to questions put by Prof. W. M.
Davis, said: The limestone boulders are twelve miles east of Cody, opposite
the mouth of Shoshone Canyon. I doubt if boulders were transported down
a hypothetical slope as sketched by the President on the black-board, but they
seem to have been carried across the Eocene filling of the basin to the east of
the mountains previous to the dissection of the basin deposits,
LI—BULL, GEOL, Soc, AM., VOL, 23, 1911
732 ABSTRACTS OF PAPERS
EVIDENCE OF THREE DISTINCT GLACIAL EPOCHS IN THE SAN JUAN
MOUNTAINS OF COLORADO
BY WALLACE W. ATWOOD AND KIRTLEY F. MATHER
(Abstract)
Abundant evidence of two distinct Glacial epochs has been reported by
several investigators from various mountain ranges in the western portion of
the continent. During the past season glacial deposits have been examined and
mapped about the margin of the San Juan Mountains, which deposits have been
interpreted to indicate an epoch of glaciation distinct from the two later
epochs that have been clearly recognized in the history of the range.
For convenience, the three distinct epochs are referred to, beginning with the
oldest, as “San Juan,” “Big Horn,” and “Uinta.”
The composition, distribution, and topographic relations of the San Juan
glacial drift indicate that this earliest known epoch was separated from the
Big Horn Glacial epoch by a much longer time than the Big Horn was sepa-
rated from the Uinta. The two later epochs appear to have been separated by
a much longer time than has elapsed since the last disappearance of glacial ice
from the range. The San Juan Glacial epoch is so far removed from the
present time that the glacial deposits of that epoch are found at but a few
places, where conditions were most favorable for their preservation.
There are reasons for believing that the San Juan Glacial epoch may have
been characterized by small ice-caps among the western ranges rather than by
Alpine glaciers, which were the prevailing type during the Big Horn and Uinta
epochs. ,
There are good reasons for believing that the San Juan epoch preceded the
development of the great canyons among the mountains, and therefore that
much of the sculpturing which has given form to the scenic features of the
range is inter- and post-Glacial in origin. The time relation of the epochs of
glaciation to other events in the physiographic history of the range was dis-
cussed.
GLACIAL INVESTIGATIONS IN MINNESOTA IN 1911
BY FRANK LEVERETT
(Abstract)
A sheet of old calcareous drift deposited by an ice-sheet radiating from
central Canada covers nearly all of Minnesota and extends into western Wis-
consin. The prominent moraines of western Minnesota, named by Upham
Itasea, Leaf Hills, and Fergus Falls, were formed in the order named, as is
shown by the glacial drainage from them. The rock constituents of these
moraines show remarkable disintegration that suggests a possible pre-Wiscon-
sin age. After these moraines were formed by the ice radiating from central
Canada, there followed an ice-movement radiating from the high tableland
northeast of Rainy Lake. This moved across the northern ends of the above-
named moraines and extended a few miles beyond the portion of the Mississippi
above Saint Paul. This produced the so-called “red drift.” After this ice-move-
ment waned, there followed a re-advance of the ice-sheet radiating from central
Canada which had its main axial movement through the Red-Minnesota-Des
GLACIAL INVESTIGATION IN MINNESOTA IN 1911 733
Moines Valley, but which also extended southeastward across the portion of
the Mesabi Range west from Hibbing, Minnesota, and spread to the left and
right in a basin which divides its drainage between the Saint Louis and Mis-
sissippi Rivers. This ice-movement deposited the so-called “gray drift” of the
Minnesota Reports. It forms only a thin veneer on the portions of the Leaf
Hills and Fergus Falls moraines which it overrode, and it failed to cover all
of the Leaf Hills moraine. The correlative position of the Lake Superior Lobe
is found to have been but little beyond the western end of the present lake, in
Carleton County, Minnesota. A large glacial drainage line opened a great
valley along the Saint Louis between Floodwood and Carleton, but was there
turned southwestward because of the presence of the Superior lobe. The rela-
tions of this latest ice-movement from central Canada to the Glacial Lake
Agassiz are such as to make necessary a radically different interpretation
from that given by Upham in his monograph on Lake Agassiz.
DISCUSSION
Mr. J. B. Tyrrect said: Mr. Leverett’s paper can not but be of interest to
every student of glacial geology in America, and especially to those who have
beeh working in Canada, where the three great centers of ice-dispersion are
located from which the ice traveled southward into the United States, for he
has shown another point of connection between the Keewatin Glacier to the
west and the Labradorean glacier to the east, through a large drainage chan-
nel from the former to the latter.
The presence of this drainage channel would appear to show clearly that the
southern lobe of the Keewatin Glacier was of the same age as the Superior
lobe of the Labradorean glacier, but I do not see why this should modify very
materially the explanation of the formation of Lake Agassiz as given first by
Mr. Warren Upham and afterwards somewhat modified by myself.”
It is quite probable that this lake had its beginning when the latest stage
of the Keewatin Glacier began to retire northward, and it is possible that the
water followed this glacier northward as far as the northern boundary of
Minnesota, but it is also quite clear that as the Keewatin Glacier retired
northward the Labradorean glacier advanced from the east into the basin of
Lake Winnipeg, in many places as far as its western shore, though at this
time it does not appear to have crossed the strip of land between Lakes
Winnipeg and Manitoba, or to have reached the Manitoba escarpment to the
west of the latter lake, but it terminated in a moraine which is now repre-
sented by islands in Lake Winnipeg and points on its western shore.
For greater definiteness this line of islands and stony points may be called
“The Winnipeg moraine.” This Winnipeg moraine was then the western or
southwestern, termination of the Labradorean glacier in its last advance into
Manitoba. There is no question whatever about its existence and about the
manner of its formation. The strie of the Labradorean glacier are general
on the rocks down the east shore of Lake Winnipeg, where they have been
beautifully preserved by the overlying covering of lacustrine clays deposited
on the floor of Lake Agassiz. In some few places the earlier strive of the Kee-
watin Glacier have been preserved in depressions in the rock surface, which
*J. B. Tyrrell: The Genesis of Lake Agassiz, Journal of Geology, vol, 4, 1896, pp,
811-815.
734 | ABSTRACTS OF PAPERS
are elsewhere completely covered by scorings made by the later Labradorean
glacier. To the west of the Winnipeg moraine the striations on the rocks
have been formed exclusively by the Keewatin Glacier from the north and
northwest.
The lake itself, at all events for the greater portion of its existence, was
bounded to the east by the front of the Labradorean glacier, and to the north
py the front of the Keewatin Glacier. :
The relationship of these two glaciers is beautifully shown by a section at
the mouth of the Saskatchewan River, where 12 feet of stratified Lake Agassiz .
clays lie between the till of the Keewatin Glacier and that of the Labra-
dorean glacier.
Lake Winnipeg is the diminished representative of Lake Agassiz, and even
now it has but a precarious existence, for it is bounded to the north by a cliff
of lacustrine clays. The outlet from the lake accidentally began where this
clay was shallowest, near its northeastern extremity, and over a bottom of
hard granitoid rocks, but if at some time the outlet should change to a posi-
tion farther west, where the clays are thicker and the underlying rock is at a
greater depth, the lake might very easily be more or less completely: drained
and we would have the Red River fiowing down through the bottom of the
basin that is now covered by the waters of Lake Winnipeg.
Mr. WarrkEN UPHAM contributed the following remarks, which were pre-
sented to the Society at the meeting by Prof. Lawrence Martin: The con-
clusions of Mr. Leverett differ so much from my general view of the history
of the glacial Lake Agassiz, presented in Monograph XXV of the U. 8. Geo-
logical Survey, that I am moved to endeavor here to present friendly com-
ments showing how I regard some of his views and arguments. He discrim-
inates, as the abstract states, three sheets of the drift in northern Minnesota
of different ages; but, instead, I consider them as practically conteémpo-
raneous in deposition, representing a tendency toward lobation where con-
tiguous parts of the broad ice-sheet, confluent together, had respectively
broad glacial currents from the northwest, north, and northeast, each of these
somewhat lobate contemporaneous ice-fields bringing drift from the areas
whence its currents came. Therefore the drift from the northwest is calca-
reous, while the drift from the north and northeast, the latter colored reddish
by the red sandstone and shales of the Lake Superior basin, has little or no
limestone. When the ice boundary was melted back at the end of the Glacial
period, its marginal moraines, formed at any times of halt or readvance in-
terrupting the general departure, were made up by whatever drift was in the
adjoining past of the ice-sheet, so that our series of marginal moraines, in
crossing Wisconsin, Minnesota, and the Dakotas, passes continuously across
the several diverse drift sheets. Much of the glacial drift was borne along in
the basal quarter or fifth part of the thickness of the ice-sheet, up to heights.
of 1,000 feet or more above the land surface, as shown by the esker of Bird’s
Hill, near Winnipeg, described in my Geological Society of America paper
two years ago. Decaying granitic and other feldspathic rocks, deeply weath-
ered before the Ice Age, yielded much drift and abundant boulders and
smaller rock fragments, shaped by the glacial erosion and held in shape while
frozen, forming a large proportion of the older drift and of the lower and
most abundant englacial boulders, small fragments and fine drift, to be worn
GLACIAL INVESTIGATION IN MINNESOTA IN 1911 735
off by the rasping ice. These fresher drift materials were carried forward
in the ice-sheet to attain even higher levels than the older decayed drift. At
the final melting such fresh drift on some areas was deposited as “a thin
veneer,” to use Mr. Leverett’s words, upon the older general drift sheet and
on its accumulations in the great marginal moraines, all these diverse types
of the drift being laid down at the time of the melting away of the ice-sheet.
The most remarkable contrast between Mr. Leverett’s views and mine comes
in his assertion that our grand moraines of northern Minnesota were amassed
during a stage of glaciation wholly antedating the existence of Lake Agassiz,
and that a relatively late ice accumulation and readvance spread over these
abundant, steep, and high morainic hills without smoothing them down,
depositing upon them a veneer of the latest fresh gray till. The late lobe of
the ice-sheet stretched southward from the Red River valley to the vicinity
of Des Moines, in central Iowa, and its departure was attended by the glacial
Lake Agassiz, growing. gradually north to the sites of Lake Winnipeg and the
Saskatchewan River. Differing from Mr. Leverett, I feel sure that our mas-
Sive Minnesota moraines were formed contemporaneously with the existence
of the great glacial lake and with its gradual extension northward, and my
opinion is that his veneering of fresh gray drift is merely the highest part of
the englacial drift, massed on the moraines at practically the same time with
their formation in the main part from lower and older englacial drift.
Mr. LEVERETT, in reply, said: The suggestion made by Mr. Tyrrell, that
southwestward-bearing strive in eastern Manitoba indicate that the latest ice-
movement was from the northeast, is perhaps a correct one for that region.
But in northern Minnesota the strie with a southwestward bearing appar-
ently pertain to the ice-movement that deposited the red drift. The ice which
later came in from the northwest and deposited gray till over the red drift
did not efface all the striz of the earlier movement. This probably was due
to the slight abrasive power of the clayey drift material which # carried.
GROOVED AND STRIATED CONTACT PLANE BETWEEN THE NEBRASKAN AND
KANSAN DRIFTS
BY J. ERNEST CARMAN®
The paper describes the unique feature of a grooved and striated contact
plane between the Nebraska (pre-Kansan) and Kansan drifts. Both sides
of the contact plane are striated. Neither side is the mold of the other.
The possible explanations are considered and the conclusion reached that
glaciation produced the feature.
NEBRASKAN DRIFT OF THE LITTLE SIOUX VALLEY IN NORTHWEST IOWA
BY J. ERNEST CARMAN?‘
The paper traces a farther extension of the Nebraskan drift and compares
the Nebraskan and Aftonian deposits of this region with those along the Mis-
souri River.
’Introduced by George F. Kay.
#Introduced by George F. Kay.
736 ABSTRACTS OF PAPERS
Mr. FRANK LEVERETT called attention to the fact that in an unpublished
paper read before this Society in December, 1904, he had described glaciated
surfaces of the sort noted in Mr. Carman’s paper, observed on the stones
imbedded in the till of drumlins in the northern part of the southern penin-
sula of Michigan. These observations in the drumlins show that it is not
necessary that the underlying drift should become cemented or indurated
before such strife are produced, and that the striation may go on in the
course of deposition of a single drift sheet. In the locality discussed by Mr.
Carman there should be conclusive proof outside of the glaciation of the till
surface that the underlying till is markedly older than the overlying deposit.
ON THE PRE-GLACIAL MIAMI AND KENTUCKY RIVERS
BY N. M. FENNEMAN
(Abstract)
Two hypotheses are entertained concerning the regional preglacial drain-
age in southwestern Ohio and adjacent States: one, best stated by Prof.
Joseph J. James, that this drainage was southwestward along the course of
the present Ohio; the other, presented by Mr. Girard Fowke, that the Ken-
tucky River flowed northeastward from its present mouth along the line of
the Ohio and Miami rivers, reversed, to join a great west-flowing trunk stream
which may be regarded as an extended preglacial Kanawha. The criteria for
discrimination consist in (1) the depth of the rock surface along present and
former stream courses; (2) local differences in the width of the Ohio Valley
between bluffs, especially certain narrows near Cincinnati and one at Madi-
son, Indiana; (3) the angles at which tributaries join the present master
streams. From newer data on (1) it appears impossible that the drainage
at the time referred to could have been northward from southwestern Ohio.
There is no evidence of subsequent crustal warping. The rock surface de-
clines at least 350 feet from west central Ohio to the mouth of Kentucky
River, but is apparently decidedly higher below that point at Madison, Indiana.
It is possible that local Pleistocene changes may have made a new valley
there. Under (2) the chief point at issue is the narrows at Madison, which
are not adequately accounted for by hardness of rocks, because there are
other features of youthful drainage. This strengthens the supposition that
the preglacial Ohio made a (not yet discovered) detour around Madison.
The facts under (3), while not alone conclusive, favor southwestward drain-
age as at present (Fowke says the opposite). On the whole, the great point
in favor of Fowke’s theory is the narrows and elevation of the rock surface
at Madison, but the slopes of the rock surface in western Ohio constitute an
insuperable objection to this theory, except by assuming notable crustal move-
ments of which there is no evidence.
RECENT STUDIES OF THE MORAINES OF ONTARIO AND WESTERN NEW YORK
BY FRANK B. TAYLOR
DISCUSSION
Prof. H. L. Farrcuinp asked if the author had determined the direction of
outflow of the waters drained away from the insular area or the tract of
CLOSING PHASE OF GLACIATION IN NEW YORK 737
exposed land surrounded by the ice-sheet. In an unpublished paper describ-
ing the glacial waters of the Mohawk and Black valleys it is shown that the
high Adirondacks were at one time in the waning of the Labradorean ice-
sheet exposed as bare highlands while surrounded by ice. The Hudson ice
lobe and the Ontario lobe were yet united by a neck or strait of ice in the
Mohawk Valley, and the drainage from the Adirondack area was southward
across the strait of ice into the headwaters of the Susquehanna River.
CLOSING PHASE OF GLACIATION IN NEW YORK
BY H. L. FAIRCHILD
(Abstract)
As the Labradorean ice-sheet melted away from the north border of New
York State, it allowed the water of the ice-bound Lake Iroquois to escape at
Covey Hill Gulf and to pass around the northeast slope*of the Adirondack
highland. Being confined and directed by the ice-border, this stream-flow
produced the extensive areas of bare rock in the towns of Mooers, Altona,
and Beekmantown, formerly described by Woodworth.® The later stream-
flow along the Altona rocks determined the level of a narrow lake lying north-
westward, into which Lake Iroquois was lowered by the waning of the ice-
front on Covey Hill, and for a time this lake succeeded Iroquois in the Onta-
rio basin. It is proposed to call this water Lake Emmons (after Ebenezer
Emmons, whose district in the first geologic survey of the State covered this
area). The further weakening of the ice-border finally allowed Lake Ver-
mont (named by Woodworth), which had previously been confined to the
Champlain Valley, to succeed Lake Emmons, and in turn to occupy the Onta-
rio basin. -It is proposed to call this expanded water Lake Vermont-New
York. These two water planes in the Ontario basin, inferior to [roquois, are
represented chiefiy by delta sand plains on the larger streams. Eventually
the waning of the ice east of the Champlain embayment allowed the glacial
waters to become confluent with the sea, and the sealevel waters were thus
established in both the Champlain and Ontario basins at the same time. The
height of the marine beaches about Covey Hill is 525 feet, which definitely
gives the amount of land uplift on the international boundary since the ocean
transgressed that area. Maps exhibit the glacial drainage channels, the
deltas, and the shorelines of the three water planes in the Champlain dis-
trict and the four planes in the Ontario district.
DISCUSSION
Dr. J. W. Srencer: The first survey of the Iroquois beach in northern New
York was made by myself. The continuous shoreline could be traced to only
a few miles east of Watertown, where I measured it 730 feet (subsequently
by Fairchild at 733). Beyond, I found a series of magnificent deltas and
sand plains. These were measured and regarded by me as the continuation
of the Iroquois beach. Dr. Gilbert and I went over the field together. He
regarded them as belonging to separate glacial lakes. Now Professor Fair-
child extends my original surveys farther east, although shore features are
5 New York State Museum bulletins, 83, 84.
738 - ABSTRACTS OF PAPERS
here different from those south of Watertown. Regarding the marine beach
of Gilbert Gulf, there are no marine shells, the calculated plain is too high
for sealevel, and the distinct deposits of marine shells are not of identical
epochs. Therefore there is no ground for the author’s pronouncement of
their marine origin.
East of Ogdensburg are beds of fine stratified clay with surface smoothed,
polished, and striated. It is covered with sand. Lying on the clay are a
very few small erratics, while no stones occur in the sand. This suggests
that a glacial advance occurred after the clay beds had been deposited, but
before the changed conditions arose which permitted the later accumulation
of sand.
INTERMINGLING OF PLEISTOCENE FORMATIONS
BY B. SHIMEK
Published as pages 709-712 of this volume.
LOESS A LITHOLOGICAL TERM
BY B. SHIMEK
(Abstract)
The term “loess” has commonly been understood as implying a more or less
distinct division of time. The facts are that there are several loesses de-
posited at different periods, and that loess does not designate a distinct period
of time, but indicates rather a condition of deposition, as do such terms as
“sandstone,” “limestone,” and “drift.”
DISCUSSION
Mr. F. V. Emerson: Loess is forming along the Missouri in central Mis-
souri. During the dry, late summer frequent dust storms carry a yellow dust
to the bluffs, where it gathers and is easily observed on exposed surfaces. This
dust in all essentials resembles the material forming the thick loess beds.
Prof. G. FREDERICK WRIGHT: In judging of the date of the various deposits
of loess, it is important to keep in mind that throughout the entire period
through which the ice was advancing there were each summer pouring forth
from it powerful currents of silt-laden water, so that whenever there was
recession of the ice-front, great or small, there might be an accumulation of
loess which would be subsequently covered by the till of a later ice advance.
It is well, therefore, to name such deposits after the various stages of ad-
vance of the ice.
But there was par excellence a period coinciding closely with the departure
of the Iowa ice when silt-laden waters were so superabundant as to lead to
the building up of the loess deposits along the Missouri and other rivers
which have been especially under consideration. Here, as in China, there
Was a special period when the accumulation of loess exceeded its ablation.
Both here and in China the erosive agents are now in the ascendant, so that
LOESS A LITHOLOGICAL TERM 739
the loess is being transported to lower levels to be deposited along the flood-
plains of the present streams and largely into the ocean itself. Whatever
agency the wind may have had in distributing the loess, it was, in America,
glacial-laden streams which brought the material into the vicinity of the
present large deposits.
Mr. FRANK LEVERETT: Professor Shimek’s suggestion that the name Sanga-
mon should be extended to the loess deposit that overlies the Sangamon soil
does not seem to me a step in the right direction. The Sangamon soil ap-
pears to have been developed under cool, and possibly humid, conditions which
followed somewhat closely the Lllinoian stage of glaciation, and in which
‘decay of organic matter in the soil did not keep pace with plant growth. At
that time there seems to have been relatively little dust im the air, or a con-
dition unfavorable for loess deposition. This in time gave place to a warmer
and probably less humid condition under which dust-laden winds transported
and deposited the loess. The earlier phase in which humus accumulates dom-
inated should be distinguished by a separate name from the later phase in
which loess deposition dominated. Certain Russian geologists have made a
clear separation of this sort and have named the earlier humus-forming
phase the forest phase, and the later loess-depositing phase the steppe phase
of the interglacial stages.
GROS VENTRE SLIDE
BY ELIOT BLACKWELDER
(Abstract)
In the Gros Ventre Valley of western Wyoming a part of the slope has been
quietly moving down toward the river for several years. In many respects the
operation is suggestive of glaciers. The slide was described, its history sum-
marized, and the geological conditions responsible for it were pointed out.
CENOZOIC HISTORY OF THE WIND RIVER MOUNTAINS, WYOMING
BY L. G. WESTGATE AND E. B. BRANSON
(Abstract)
A preliminary account of the successive peneplains, partial peneplains, and
terraces of the southern part of the Wind River Mountains, the preglacial
gravels capping some of the terraces, and the relation of the terraces to de-
posits of an earlier and a later glaciation.
STABILITY OF THE ATLANTIC COAST
BY DOUGLAS WILSON JOHNSON
(Abstract)
The results of the Shaler Memorial Investigation of shoreline changes along
the Atlantic coast indicate that there has been no appreciable subsidence of
740 ABSTRACTS OF PAPERS
this coast within the last few thousand years. The phenomena which seem
to indicate recent subsidence appear to fall into three groups: (1) Fictitious
appearances of subsidence which are produced by wave action on a retro-
grading shoreline without any change in thie level of land or sea; to this
group belong many instances of submerged stumps, peat exposed at low water
on the seaward side of barrier beaches, erect trees recently killed by the in-
vasion of salt water, etc. (2) Phenomena produced by a local rise in the
high tide surface, due to a local change in the form of the shoreline, unac-
companied by any general change in the relative level of land and sea; in this
group may be found examples of practically all phenomena ordinarily attrib-
uted to a recent subsidence of the land. (3) Phenomena produced by an
actual subsidence of the land or rise of the sealevel which occurred some
thousands of years ago; in this group belong many of the deeply buried peat
deposits and submerged stumps. The evidence of coastal stability consists of
(1) the form and position of successive beach ridges, the oldest of which were
built by the waves thousands of years ago, yet later than the deeply buried
peat deposits; (2) the position of abandoned marine cliffs on which the waves
can not have worked in recent time, and (3) the absence of a fringe of dead
trees on those portions of the coast which are exposed neither to direct wave
attack nor to local fluctuations of the high tide surface. It is concluded, with
reference to the Atlantic coast, that the land can not have subsided as much
as a foot within the last century; that there can have been no long continued
progressive subsidence at so high a rate as one foot per century, within the
last few thousand years, and that no evidence thus far available can be re-
garded as satisfactory proof of any degree of recent subsidence, either spas-
modic or progressive.
DISCUSSION
Dr. C. A. Davis: The physiographic evidence to be gathered on the exposed
shores is not such as to show slight changes of level as the range of the tides
is so great; hence recent subsidence can neither be proved nor disproved by it.
While we have the possibility of a general elevation of the tidal surface be-
cause of changes in the shores of the Atlantic, there is no evidence that this
has occurred or that such elevation is going on either in tidal records or
elsewhere. ‘The evidence of the salt marshes that subsidence is going on, since
it is to be presented in a paper to be read at this meeting, will not be men-
tioned now, but it may be said that at Nantasket Beach there is a small area
of salt marsh which shows recent change of level, in that if there had been
stability for as much as 1,000 years it could not exist as a salt marsh, be-
cause the plant remains would have built up above the reach of the tides.
Four or five miles southwest of Nantasket is an area of salt marsh with
stumps of trees in place more than 2 feet below the level of ordinary high
tides, and partly buried in salt marsh peat, which must have been formed
by the gradual change of the relation of the high tide to the bottom. No
sudden change in the relation would account for this accumulation, and the
change has not yet ceased. The tidal waters find their way to this area by
tortuous channels. and any change of tidal level on the marsh must have
been accompanied by greater ones at the beach, as the tidal wave has more
direct access to it.
STABILITY OF THE ATLANTIC COAST (41
Dr. J. W. SepenceER: In support of the present stability of the land and sea,
I have found from analysis of the daily fluctuation of the Great Lakes that
there has been no change of even a tenth of an inch since 1850-1855. (See
chapter xxxi and appendix, “The Falls of Niagara,” Geological Survey of Can-
ada, 1907.)
Prof. A. C. LANE referred to the work of J. R. Freeman for the Charles
River Commission and since, and said that his observation of the Nantasket
region referred to led him to believe a subsidence of 5 feet between the for-
mation of the first connecting beach and the present might be allowed.
Dr. H. B. KiimMeEL: Since the results of Professor Johnson’s observations
have come to my attention I have been very much interested in determining
the origin of the unqualified assertion so frequently seen in text-books, that the
coast of New Jersey is subsiding at the rate of 2 feet per century. I found
that in 1857 Prof. George H. Cook, then professor of geology at Rutgers Col-
lege, New Brunswick, New Jersey, read a paper before the American Asso-
ciation for the Advancement of Science, in which he set forth the various
facts which led him to conclude that the coast of New Jersey had suffered a
long-continued and slow subsidence, and that this downward movement was
still in progress. At the close of his paper he cited a number of facts bear-
ing on the rate of subsidence, and he concluded that “we may, with some
degree of probability, state the average subsidence in the district where the
observations were made as two feet in a century.” Referring to facts in
relation to the rate of subsidence, his final statement was, “It is not unlikely
that other and more numerous observations may give a different result.”
On the basis of this paper, published in the American Journal of Science in
November, 1857, the present subsidence of the New Jersey coast at the rate
of 2 feet per century was apparently accepted as demonstrated, and state-
- ments to that effect were published thereafter in Dana’s Manual of Geology,
at first on the authority of Professor Cook, and later without authority, as a
well known and established fact.
In 1885, in the report of the State Geologist of New Jersey for that year.
Professor Cook reviewed all the data in his possession bearing on changes
along the New Jersey coast, and while he still held the opinion that the coast
was sinking, he stated that it was “at a rate which is not yet quite definitely
established.”
Two or three years later, after the topographical survey of the State was
completed, certain facts in regard to the relative level of high tide in the
ocean and in the lagoons behind the barrier beaches were brought to Pro-
fessor Cook’s attention, and he then realized that some of the facts upon
which he had very strongly relied as proving present subsidence were prob-
ably to be differently interpreted; so that I think I am safe in saying that at
the time of his death, in 1889, he was not nearly so strongly convinced that
the coast of New Jersey is sinking at the present time as he was thirty years
earlier.
Professor JOHNSON replied as follows: Referring to Mr. Spencer’s com-
ments, I might say that it was the intention of Mr. J. B. Tyrrell, had he not
been compelled to leave early, to present certain evidence recently acquired
742 ABSTRACTS OF PAPERS
by him tending to show that there had not been any marked change in the
relative level of land and sea along the southwest coast of Hudson’s Bay
within the last two or three hundred years; certainly nothing like 5 feet in
that length of time. His evidence is based on a comparison of carefully
‘made maps. If his interpretation is correct, it is an interesting example of
coastal stability farther north than our observations have extended.
Replying to Dr. Davis, it is true that the physiographic evidence of coastal
stability is not as sensitive as one could wish. All physiographers will recog-
nize the difficulty of proving absolute stability by beach ridges which may
vary in height several feet. On the other hand, the physiographic evidence
is very reliable and seems to prove conclusively that there can have been no
marked subsidence of the coast for several thousand years; certainly the
deeply buried peat can not possibly be explained on the theory of recent sub-
sidence, for the beach ridges prove that the coast can not have subsided more
than a very few feet at most, whereas the peat descends to much greater
depths.
I believe I have never held that there can have been no subsidence what-
ever in recent times. I have always held that the physiographic evidence did
not preclude the possibility of a slight subsidence in the last few thousand
years. On the other hand, I have held, and still believe, that there is no
reliable evidence that even a slight subsidence has occurred in recent times.
Tidal fluctuations and other shore changes will account for the apparent evi-
dences of subsidence. ;
Dr. Davis seems to believe that only gradual changes in the relative levels
of land and sea could account for the dead stumps he has described, and that
therefore the theory of tidal fluctuations will not account for them. I should
have said that inasmuch as changes in the form of the shore often take place
gradually, the local rises of the high tide surface which produce apparent
subsidence also take place gradually. Only in exceptional cases is the rise
so sudden as in the Scituate case which I’ described.
SOME COASTAL MARSHES SOUTH OF CAPE COD
BY CHARLES A, DAVIS
(Abstract)
A report on a continuation of the work on salt marshes in the vicinity of
Boston, the results of which were reported at the Boston meeting in 1909.
The structure of salt and brackish marshes on the south side of Cape Cod
and on Long Island is described, and the evidence this bears in favor of recent
coastal subsidence is discussed.
DISCUSSION
Prof. J. B. WoopwortH remarked on the apparent validity of the argument
for subsidence based upon the structure of Spartina patens marshes and the
contradictory evidence as to a very recent subsidence of the coast pointed out
by Prof. D. W. Johnson from his finding successive beach crests of ancient
COASTAL MARSHES OF CAPE COD 743
and modern date at the same level. He inquired what Dr. Davis would offer
as an explanation of the failure of the older beaches to show subsidence.
Prof. A. W. GraBau asked for a statement as’ to the depth of the peat de-
posits in the Long Island region and the rate of growth of the salt peat.
Dr. Davis replied: Two hypotheses may account for the lack of apparent
accord in the physiographic evidence of the beach and other phenomena cited
with the botanic evidence of subsidence: (1) The beach phenomena may not
be so old as supposed. (2) They may have been formed by high storm tides
long ago to a level which has been brought down to the present one by sub-
sidence, as trees are apparently brought down within reach of tidal waters
in the 200 to 500 years of their lives. The greatest subsidence found in the
brief studies in Long Island was about 10 feet. The only records showing
rate of subsidence found were in the vicinity of Boston at the end of the field
season. In two localities the turf of salt marshes along long-established rail-
Ways was found to contain coal cinders from locomotives in the upper 3 or 4
inches. One of the lines had introduced the use of coal in its locomotives in
1861, and by 1865 had equipped all of its locomotives for burning coal.
ORITERIA FOR THE RECOGNITION OF ANCIENT DELTA DEPOSITS
BY JOSEPH BARRELL
Published as pages 377-446 of this volume.
ANCIENT DELTA DEPOSITS
BY A. W. GRABAU
(Abstract)
After a brief reference to the pre-Cambriec or early Cambric delta fan of
the Pacific province and the Torridon of Scotland, the following were discussed
with especial reference to their stratigraphic and paleontologic characters
and their bearing on paleogeograpbhy :
The late Ordovicic and early Siluric fans of the Appalachian region.
The Shawangunk dry delta fan and its relationship to the Salina desert.
The Esopus delta and its relation to the Oriskany deposits.
The early Devonic talus breccia of Michigan and western Ontario.
The Old Red of Scotland and the Catskill group.
The Pocono, Mauch Chunk, and Pottsville.
The Triassic fans of America and western Europe.
MISSISSIPPIAN DELTA IN THE NORTHERN NEW RIVER DISTRICT OF
VIRGINIA
BY E. B. BRANSON
Published, under the title “A Mississippian delta,” as pages 447-456
of this volume.
T44 ABSTRACTS OF PAPERS
DISCUSSION OF THE PRECEDING THREE PAPERS
Dr. J. M. CLARKE referred to the continuous presence of Devono-Carbonifer-
ous continental deposits on all the eastern frontage of the Appalachians, espe-
cially to the delta work presumably of the Saint Lawrence River, represented
by the Bonaventure formations of the Gulf of Saint Lawrence.
Dr. Davip WHITE: The Pocono formation is essentially a unit, though
erosionally disconnected in its extension from southwest Virginia to the
Mauch Chunk region of Pennsylvania. Along its easternmost belt it consists
of well washed and comparatively regular gray grits and sandstones, with
interbedded shales and coals. The character and extent of the sandstones
suggest coastwise distribution and differentiation of the material. The pres-
ence of coals, which throughout the greater part of the eastern border of the
existing Pocono zone are nearly if not quite of workable thickness, and the
occurrence, at many points at least, of roots in their place of growth in the
underclays, demonstrate extreme shallowness of water cover at the time of
deposition of the coals. The relative narrowness of the longitudinal zone of
typical Pocono sandstones and coals points either to the existence of an
estuary extending from the Tennessee region northward along the Appa-
lachian trough at this stage of the earliest Mississippian or to the presence of
barriers separating and essentially isolating narrow and shallow eastern
basins from the broader marine expansion on the west. In the former case
the narrow estuary, which seems more probable, was the starting point for
an extensive northwestward transgression, with the early development of
marine conditions. The rapid thickening of the beds toward the east (shore-
ward) and the increase of coarse detrital matter in the same direction har-.
monize with the recognized existence of drainage from the eastern land out
into the basin. The latter, as shown by the coal deposition, included a broad
filled zone standing at times at or above sealevel. It is probable, however,
that the areas of actual Pocono “delta” are now obliterated by erosion.
Throughout most of the region or zone of typical Pocono sedimentation
marine fossils have not been found. An exception is the Broad Top field,
where brachiopods and other marine mollusks occur in the lower part of the
formation, which there maintains a thickness of over 1,000 feet, though the
formation is very much reduced at the Allegheny front.
There is no evidence that the Mississippian sea was at any time deep in
the Appalachian trough, a feature already pointed out by Ulrich. The pres-
ence of conglomerates, of old soils, breccias, and land plant remains at various
horizons in different areas of the post-Pocono Mississippian, indicates a num-
ber of intervals and regions of exposure of portions, at least, of the trough.
These episodes will no doubt eventually be fitted into a somewhat complicated,
though very interesting, history of the Appalachian trough during Mississip-
pian time.
Dr. G. W. StTose: In discussing Mr. Branson’s paper, I wish to refer to the
occurrence of the Price sandstone in the Abingdon quadrangle, Virginia, some
30 miles to the southwest. There the Price has a rather uniform thickness
of about 600 feet for 50 miles along the strike, showing no thickening due to
deltas. There is a marine Mississippian fauna in the upper half of the for-
DELTA DEPOSITS 745
mation and thin coals only at the very top. It is concluded that these sands
were derived from deltas, such as the one described by Mr. Branson, of
streams heading in the older rocks to the east and flowing across a coastal
plain to the inland sea, and there distributed along the shore by shore cur-
rents.
Mr. ArTHUR KEITH called attention to a statement by Professor Grabau that
a certain type of cross-bedding characterized continental deposits, cited the
common occurrence of cross-bedding in marine and continental beds, and re-
quested Professor Grabau to inform the Society as to the difference seen be-
tween marine and continental cross-bedding. Such distinctions would be very
useful as criteria on account of the easy recognition of cross-bedding.
Prof. E. T. WuHerry: At the northern edge of the Triassic in eastern Penn-
sylvania conglomerates occur which, judging from their character and dis-
tribution, are to be regarded as delta deposits.
Dr. H. B. KiiMMEL raised the question whether a distinction was not to be
made between ancient alluvial fans wholly subaerial in origin and formed
wholly independent of bodies of standing water and true deltas. Some of the
instances of deltas cited in the discussion seem rather to be alluvial fans
similar to those now being formed in the west at the foot of high mountains.
The authors made the following replies:
Professor BARRELL: A study of criteria to separate the submarine and sub-
aerial deposits of deltas brings out clearly the need of more refined compara-
tive studies of modern sedimentation under a variety of conditions. It is
evident, however, that certain criteria are not to be used according to their
mere presence or absence, but rather according to their specific characters and
dominance. Cross-bedding may be cited as an example, present in marine,
fluviatile, and eolian sands, but presumably showing distinctive characters in
each case. :
In reply to the comment of Dr. G. I. Adams as to the apparent confusion
which is being introduced of marine formations with delta deposits, it may be
said that by definition deltas involve both subaerial and subaqueous phases,
since they are built against permanent bodies of water. On the other hand,
marine beds of mud or sand should not be regarded as belonging to deltas un-
less there is evidence that they passed on the landward side into synchronous
fluviatile deposits. There is no inherent distinction between the bottomset
beds of a delta and the offshore bottom deposits opposite a river mouth, where
deltas have been unable to form. Delta conditions involve the conception of
certain relations between contemporaneous fluviatile and offshore deposits,
not the nature of the beds themselves, for these are merely fluviatile and
marine.
Professor GRABAU: The two types of delta—sea-shore and subaerial fan—
are probably to be recognized in the older deposits. Of the sea-shore deltas,
in part subaerial, the Bald Eagle, Juniata, Tuscarora, and perhaps Shawan-
gunk and Pottsville. The Longwood is most probably a subaerial fan, as
there are no known marine parts of this deposit. The same is true of the
746 ABSTRACTS OF PAPERS
Triassic deposits of eastern and western North America, though those of west-
ern Europe may perhaps come in part under the first group.
The distinction between marine and continental types of cross-bedding is
not easy, chiefly because our observations are too limited. We have, how-
ever, the following: Hobbs has shown that cross-bedding of a torrential de-
posit, such as the Guadix and related formations of comparatively recent ori-
gin, consists of a series of diagonal and horizontal beds many times repeated,
and the diagonal beds all dipping in some one direction, while the successive
horizontal and diagonal series are of moderate thickness, perhaps not over 6or 8
feet, and not much less. Such cross-bedding has not yet been described from
undoubted marine strata, nor is it conceivable how it can be formed under the
sea. Walter Huntington and others have shown that the cross-bedding, with
the successive series dipping in all directions and separated by erosion planes,
is characteristic of eolian deposits due to migrating ripple-marks, and can pro-
duce this structure on a large scale under the sea, except in sand-bars, when it
would have only a linear extent. So far, then, as we now know, cross-bedding
on a large scale, except when of only lineal or limited extent, is character-
istic of continental deposits. Fossiliferous eolian deposits are illustrated by
the Lunegarth limestone.
STRUCTURE OF ESKER FANS EXPERIMENTALLY STUDIED
BY T. A. JAGGAR, JR.
(Abstract)
Deltas formed by miniature cavern torrents were shown and cross-sections
made by slicing them. The conclusions arrived at concern the effects of sheet-
floods, of a raised or lowered lagoon level, of variation in load of detritus and
variations in velocity and volume of current. These effects appear in the sym-
metry and asymmetry of ground plan of deltas and in the relations of topset
and foreset beds.
‘EFFECT OF RAPID OFFSHORE DEEPENING ON LAKE-SHORE DEPOSITS
BY RUFUS MATHER BAGG, JR.
(Abstract)
Local beach pebble deposits on the shore of Little Sister Bay, near Ephraim,
Wisconsin, on the east side of Green Bay, consist of Silurian (Niagara) lime-
stone pebbles beautifully rounded by wave action in a protected cove, where the
water grows deep very rapidly offshore. No similar occurrence is to be found
anywhere in the immediate neighborhood along this shore where similar con-
ditions prevail. In all other sections the flat limestone fragments remain in
more or less of their original condition or but slightly water-worn.
STRUCTURE OF THE HELDERBERG FRONT
BY A. W. GRABAU
(Abstract)
The Helderberg front is the northern extension of the westernmost belt of
the Appalachian folded area, left after extensive erosion. The former extent
STRUCTURE OF THE HELDERBERG FRONT T47
east of the Hudson is partly indicated by Becraft Mountain and Mount Ida.
The basal part is of folded Hudson strata unconformably succeeded by late
Siluric, showing various phases of overlap. The Appalachian folds are of the
usual asymmetric type, while the range from near Rosendale to Catskill and
beyond is complicated by one or more pronounced overthrusts. The first of
these was described by the author from Kingston, and subsequently more fully
discussed by Van Ingen and Clark. Chadwick has described a part of the
thrust at Saugerties and the author has determined its character near Catskill.
Several new sections from this last region were presented.
DISCUSSION
Prof. J. B. WoopwortH called attention to the fact that in southeastern
New England the carboniferous areas show overthrusts to the southeastward
and not to the westward. It should not, therefore, be assumed, as has been
done, that there has been everywhere in the Appalachian geological province
an overthrust as from the Atlantic basin.
SUCCESSION IN AGE OF THE VOLCANOES OF HAWAII
BY T. A. JAGGAR, JR,
(Abstract)
The plan of the Island Hawaii shows a symmetry in accordance with the
structure of the several volcanoes, and the activity of two of them, which
leads to the conclusion that there is a record of succession shown. This is at
variance with Dutton’s conclusion that no age of beginning of activity for a
given vent can be assigned. The writer not only postulates a succession in
age of beginning and closing activity in the older vents, but he argues that
Kilauea is not the youngest vent. The argument presented suggests a perma-
nent lava column continuously rising.
’
BIBLIOGRAPHY OF THE MAMMOTH OAVE
BY HORACE C, HOVEY
(Abstract)
This catalogue contains the titles (with brief descriptive notes) of all known
publications concerning Mammoth Cave and its contents, comprising descrip-
tions of its antiquities, scenic features, geology, environment, cavern fauna,
and flora.
LII—Bott. Grou. Soc. Am., Vou. 23, 1911
INDEX.TO VOLUME 23
Page
ApamMs, G. I., Delta deposits discussed
EE oe ois bo oho iv wal nn ane bosses 48, 746
AFRICA (British Bast), Physiographic
provinces and their relation to geo-
Stet) BELUCTULE. .6 estes bee as 299
AFRICAN (East) plateau, Physiography
NFER ORFS Sieve vis Siar olecchens sai 6S 49, 297-316
—mammals; W. D. Matthew...... 85, 156
AFTONIAN deposits, Sioux Falls section. 146
“Ach of Mammals,’”’ Reference to Os-
LOD. SS eee . 168
AwABEOoOUm pass, Alaska. .......3..<26. 567
ALASKA and Yukon, Differential ero-
sion and equiplanation in portions
bee 333-345
—, Glacial deposits of the continental
I PEREeEs aS cae x ols aw ersiefene oe 44, 729
—, Glaciation in northwestern... 44, 563- 570
—, Mesozoic stratigraphy of; G.C. Mar-
Loca ne +E ace eee 36, 724
Sura. River and Valley, Alaska. 566
“aia W. C., Delta deposits discussed
—, Pleistocene formations and “loess”
DUS OTE SEG 0) 0) ee ee ee 48
— ;Pre-Wisconsin glacial drift in the
region of Glacier Park, Montana.
44, 687- 708, 730
ALTAMONT moraine (The), Sioux Falls
So UO e ES 8 cae eee 150
AMI, H. M., Correlation of Paleozoic
faunas discussed by..............
—, The Ozarkian fauna discussed by.. 84
ANDERSON, F. M., Origin of sandstone
near Carson City discussed by.... 73
—, Miocene of the southern Coast
Range region of California dis-
ODER LS Oi Bi Sear nee 72
ANDERSON, ROBERT, Earth-flows de-
scribed in Science, n. s., vol. 25,
1907, p. 769, by
ANDERSSON, J. E.; “Solifluction a com-
ponent of subaerial denudation,”
URTMETUC ELI cine tse ois vs boa! 6 are 342
ANNUAL address of the President... 93-124
ARID and humid initial conditions,
trasted characteristics of..... 43-548
—-— moist topographic juvenility, Con-
trasted features of........... 548-554
—climate, Deflative scheme of the geo-
graphic cycle in an....... 49, 537-562
— stage, Ideal type of early.......... 550
ARIDITy, Essential features of. 543
ARKANSAS diamond-bearing peridotite
MELO. CIC 7. oo gicye nis wie ow 3.4
ARTESIAN well (two) records from Hat-
teras Island; Collier Cobb........ 51
ARTIODACTYLA; O. A. Peterson..... 86, 162
ASHLEY, GerorRGE H.; _ Stratigraphic
study of the Appalachian and Cen-
tral States with reference to the
occurrence of oil and gas...... 37, C20
ATLANTIC coast, Stability of....... 49, 739
ATWooD, W. .. Differential erosion
and equiplanation discussed by. 49
—, Glacial deposits east of Cody, Wyo-
ming, discussed by.........- 45, 731
—, Pre-Wisconsin glacial drift in. the
region of Glacier Park, Montana.
GINCUBBCR DY... ccc ccc eeccer ss 44, 680
Page
ATWoopD, W. W., and KirRTLEY F. Ma-
THER; Glacial epochs in the San
Juan Mountains of Colorado... 46, 732
AUDITING Committee, Election of...... 2
BaGG, Rurus MATHER, JR.; Effect of
rapid offshore deepening on lake-
shoresdeposits)s%.).. 1 ose visweriee 50, 746
BAKER, CHARLES LAURENCE; Notes on
the Cenozoic history of central
WYGHIHE. |.) «cue xs eee Bet
BARRELL, JOSEPH; Criteria for the rec-
ognition of ancient delta deposits. .
48, 377-446, 743
—, Fossiliferous conglomerates discussed
BARTON, GrorGp H., Bibliography of W.
ER NGIGSG Dy 3215 ost ac cetetahotal eestor
Basic igneous rocks, N. H. Winchell’s
SEUGIOS (Obs scant che cha ols eiare mee
BASSLER, R. S., Development of the
monticuliporoids discussed by.....
—, Devonie corals discussed by..... J oe
—, Fish fauna discussed by.......... 87
—,O. P. Hay introduced by.......... 87
—, Secretary ; Symposium on ten years’
ee ot in vertebrate paleontol-
= 8) ORO OIE ae Oe te 85, 155-266
Bien, BE. S., Correlation of Paleozoic
faunas discussed LS Ae cure Sea
Bay tery, W. S.; Peculiar iron ore from
the Dunham mine, Pennsylvania... 44
BracH of Covey Hill, Reputed marine. 475
BEEDR, J. W.; Origin of the sediments
and coloring matter of the eastern
Oklahoma Red Beds.......... 36, 723
BELT, THOMAS, quoted on the Pis- Pis
GiStricty “NiICATALUA . scious os sleles a 495
BERKELEY Meeting, Register of Fellows
AWOMVISIEOT RMAC tie echoes acus Sclaleta 75-7
BEYER, SAMUEL W., elected Councilor
Geological Society for 1912-14.. 2
ae it ela of Christopher Webber
BLD Manso Gal coeds eis ale w eiekey adhe
—— Mammoth Cave; aa Cc. “Hovey
and R. Ellsworth Call........ ore
— (partial) of paleogeography, 1900-
1912 9.8 210) 258 C_UVe awe w/e 64 2'a.8.8 & eeneevwee8e 254
a SAMIIEL POM byilicne cies ecient Parca wae 9
—-— Samuel Franklin Emmons...... 7 eee
= SAVORS Ce ee eG AS aye gta ate ak ate 34
aE NSF SONG LOTMOLO Ete tang e wikis mydad anata 219
— —— New Mexico coal fields.... 659-686
BLACKWELDER, ELiIoT; Gros ‘Ventre
STAG os ckacatarexcele Gene oe 51, 487-491, 739
BLUEFIELD formation, Mississippian
delitay Gf Py VIERIUNID. « ocr eteus ses ajeterwes 452
BoutpEerR beds of the Caney shale at
Talihina, Oklahoma; J. B. Wood-
WU OIL ALS: Sara, thes nid &a) aio hk eas 50, 457-462
Bowlb, WILLIAM; Gravity anomalies
and geological Tormiations. . src su eseiccel steustereapate 46, 463-470
CHBTONEA) Olivers eee El dysencrareueietote soteore mealies
CHELONIOIDEA, Bibliography Obnte Oa ere 219
CLAPP, FREDERICK G.; Occurrence of
petroleum associated with faults
ST UUISES sine. Buns sacar ne me ean 51, 728
CuarK, W. B., elected Treasurer Geo-
logical: Society for 1912.......... 2
—on Committee on Correspondentship. 35
CLARKE, J. M.; Correlation of Paleozoic
faunas discussed by..........+ See
—, Delta deposits discussed by..... 48, 744
—, Development of the Monticuliporoids
GISCUSSEGs view tcpa. cic ele as ebenverasin els 84
—, Fossiliferous conglomerates dis-
CUSSEM’ | BY s, «err aeuets oy eikbelassocieaniyte eae 83
—, Middle coranelon erustaceans dis-
CUSREG: 7) Wile car Seu Sons den teak cosa ate eae 84
—, Oriskany cp oaeronee of Ontario dis_
CUSSEG Pc DYiy cs cieswst-i oy hsm nueiereceterateber sts 83
: Paleontology of a voracious appetite. 83
—, "Toastmaster at annual dinner.. . 46
CLuTE, JoHN; Statement concerning
salt beds of Seneca Lake......... 481
BULLETIN OF THE GEOLOGICAL
SOCIETY OF AMERICA
Page
Coat fields of northern central New
Mexico, Stratigraphy of. --» 041-686
COASTAL marshes (some) south ‘of Cape
Cod} Charles A. Davis: 22-0 see 50, 743
— plain, British Hast Africa, The..... 299
— — investigations conducted by the
United States and State Geological
Surveys; T. Wayland Vaughan.. 82
Cops, CoLLipr; Two artesian well rec-
ords from Hatteras. Island 2. se
Ca:uR D'ALENE Lake, Origin and age of. 531
COLEMAN, A. P., Fossils of lower lime-
stone of Steep Rock series. dis-
CUSSEG “DY. «cle ve 2 ee 46, 723
—, Pre-Wisconsin glacial drift in the
region of Glacier Park, Montana,
discussed by... ...\2 eee 44, 730
COLLIE, GEORGE Lucius; Physiography
of the Hast African plateau. 49, 297-316
COLOR scheme for crystal models ;
George H. Chadwick... -.e0eee 51, 728
CoLorADO Front Range, An explanatory
description of the......... 94
CoLUMBIA River (Yakima) _ lava, "Age
OBS sss coisas hands core ieee 535
COMMITTEE on Correspondentship, “ Ap-
pointment . Of... 4-4
Dinwwe, annual Society........0...6. 46
DINOSAURS, Cretaceous and pre-Creta-
3 DE Rae aes eee 85, 204, 208
DRAINAGE lines in desert regions, De-
Melopment OF OMIZINAL. 26... oe see 555
—of Seneca Valley, Reversals of...... 480
Drirrs, Grooved ‘and striated contact
plane ashe the Nebraskan and
RL TINSRER Settee ie! vicit| ego's coe 2 5,6, 0) 47, 735
—; Neocolemanite, a variety of colema-
nite and howlite from Lang, Los
Angeles County, California....... 70
EARTH-FLOW, The Gros Ventre slide, an
PNSURY Cin, deel args tan ante wm ete tad pits 487-491
EASTMAN, C. R., Fish fauna discussed
DEY, er ibs alas Seiardhe le Bc taiapaim Site eee eee eee 87
; Jurassic Saurian remains ingested
WEEN: TAS oS is ac oi Sentaseen ont eee 87
—; Mesozoic and Cenozoic fishes... 86, 228
Sete genus Edestus discussed
BYira eh ot sumice sy aelel wtedyelertns Sop ate laine alls dea 87
EASTPORT quadrangle, Maine, Faunal
characteristics of the sediments of
MELO ihn fe, wide ch tac er oy alte panera eae ee Oke aac 352
TOGKS, GE THE <5 sn .cikos.6 crate kid cine ae 351
ELECTION of officers, Geological Society. ey
IEXMERSON, F. ‘Y., Pleistocene ‘forma-
tions and “loess” discussed by.. 48, 738
EMMONS, SAMUEL FRANKLIN, Bibliogra-
BELO Beste eo ae opae een a Se ae a 24
NIG Ae tes ets 12
EOCENE correlations to the year 1911,
Signi @sis. OF 3. visite tetas cant ance 244
, Upper, and Lower..... 237, 239
Eouric erosive activities, Toyalané and
EGUEETO) TESTOR oe) Sic: essere meres a emiete ma re ws
HOULIPLANATION in AlaSE@:....°. 5.5... .\e2 344
EROSIONAL agents under diverse ee
WIVaAIe CONGITLONS 2 a0) 0,<) = see ae 539-542
Erosion and Oxidation, Post-Glacial. 277- aps
——~ Baselevel Of \COHAN. .. 2.05 sss euieiee a's 559
—'conditions, Relation of glacial and
BUTS TUM «on eS SEES wi seis a nactial eee aiakstons 542
— (differential) and equiplanation in
portions of Yukon and Alaska;
De Lorme D. Cairnes..... 48, 333-345
—., EKolic character of regional........ 117
— in the Valley of the Great bakes<..:. 287
— (stream) south of the Saint Law-
rence-Mississippi watershed....... 2
ESKER-FANS' experimentally studied,
SETGHUIG GL sie scala cate. m ate into eres 51, 746
rraces, Significance of...........-- 285
EVOLUTIONARY evidence; S. W. Willis-
CUM Ve hee vcetae tes nla x Fe ei ans 86, 257
FAIRCHILD, HERMAN L.; Closing phase
of glaciation in New York..... 47,
—, Covey Hill revisited discussed by 3
elected President Geological Society
TT: ee chem Garcinia abies. Srgicl a oad 2
—,Moraines of Ontario and western
New York discussed by.......-.-.-. 46
—, Post-glacial erosion and oxidation
discussed RO re eer 47, 738
FANGLOMERATE, a detrital rock at Bat-
tle Mountain, Nevada; Andrew C.
TORO Sete iee eas Mintel su aishae oie ce 72
FARRINGTON, OLIVER CUMMINGS; New
minerals from the Favas of ee aan
i, 62
Fau.uts, Preliminary report of the Com- _
mittee on the Nomenclature of. 50
Faunas of the Eastport Quadrangle,
Maine, Correlation of the P aleozoic.
83, 349-352
Fayum fauna, Groups and arrangement
Rc ste ile «ae waa ihe al aaeat oaks el oreen 157
156
FELLOWS elected, 1912........cesee0 3
FENNEMAN, N. M.;: Pre-Glacial Miami
and Kentucky rivers........-- 1, 736
752
Page
FinceR Lakes, Discussion concerning.. 478
FisH fauna (A) from the Pennsylva-
nian of-Wyoming; E. B. Branson.. 87
ForerRSTE, A. F.; To what part of the
Richmond does the Medina of On-
FORRESTER, ROBERT, Mesaverda fossils
a in southwestern Colorado
FOSSILIFEROUS conglomerates; A. W.
TAROT bck bo custe eos levator e Sra taveteaene, ole 83
FossiIt invertebrates of the ‘“‘Laramie’”’
formation, southwest Colorado.... 591
— plants from central and western New
Mexico and southwestern Colorado,
Table showing distribution of.....
— plants from the ‘Laramie,’ New
RT OR ECO Abe | osiag ete ercietale Cactet O akee ores ole re 617
FossIts, Absence in deltas of......... 415
—as evidence of terrestrial deposits,
‘Perrestrial ssid --2 ewes « eee ete ere ee 443
— described by Prof. Samuel Calvin,
TGASE" OBS Soe. cote ae eae Coit te eee
—from North Cayuga and Walpole
tOWDSHINS Ontario. chine «fe 373, 375
——named in honor of Prof. Samuel Cal-
WIM Gre ote k.e oie co. ope RRS ae Se lees f¢
—of lower limestone of Steep Rock
series; Charles D. Walcott.... 46, 723
GARDNER, J. H.; Table of section of
Cretaceous rocks measured near
Durango: Coloraden:.c.% «2. ss 584-589
GEIKB, JAMES, quoted on the Great
BADGES) eek orey ates coe cera ous are tareigner arene 478
GENUS Edestus, Remarkable specimen
helongine to. the... OUD. s 2525. un eters Sienna 477
—of the Nevada hills; A. C. Lawson.. T4
—, Relation of geography to; W. M.
DY oh gE Ee Mee
eer reer eee
BULLETIN OF THE GEOLOGICAL SOCIETY OF AMERICA
Page
GEOPHYSICAL Laboratory of the Car-
negie Institute, Visit of members
EOnd 5. x's acs chee aein cite eS eee tint
GIDLEY, J. W.; Perissodactyla..... 85, 179
GILBERT, G. ke Memoir of Edwin E.
Howell by... see 46, 732
GLACIER Park, Montana, Pre-Wisconsin
glacial drift in the region, 7 eo -
4, 687-708
GLEN, L. C.; Arkansas diamond- Leen
peridotite ALTCR . ... 2515.3 ee 37,
GNEISS province, British East Africa,
4 302
Gorpon, C. H.; Onyx deposits in east
Tennesse. .... io. - 5s 5 37, 729
GRABAU, A. W., A new Trenton Crinoid
from Ontario discussed Dacca
—; Ancient delta deposits......... 48, 743
—, Coastal marshes south of Cape Cod
discussed by... ...<. 45am 50, 743
—,F. F. Hahn introduced by........ i *
—+;Fossiliferous conglomerates........ 83
—-; Notes on Devonie corals..... ee
—_, Paleontology of a voracious appe-
tite discussed by... <<<. samen 83
— ; Structure of the Helderberg
Front... ec. cc ce ee 6 eee ), T46
—, The Medina of Ontario discussed ee 83
—- Ozarkian fauna discussed by.... 84
GRAND Canyon of the Colorado River;
N.. HB. Darton.<. hee
— —, Sloux Falls section. ......:i<.. 148
KAy, ’ GEORGE F., J. E. Carman intro-
‘duced DY: sok»: ok Realal nt cce peeks, chee ae eee 47
KEITH, ARTHUR, Delta deposits dis-
CUSHEE (DY «60 sis.s tard os eee aoe 48, 74
—elected Councilor Geological So-
_ ciety for 1912-1914
"tion Ei aiehs oh afarebemeeas Tie bee 3 5, 720
519
KEYES, CHARLES R. Geareeanic cycle
in an arid imatas should its de-
velopment be by wind or water?..
49, 537-562
—j; Toyalané and Lucero; their struc-
ture and relations to other plateau
plains of the desert....... 50, 713-718
KIMBALL, J. P., Segregation of iron ores
first applied Vic Fac sent wera eid ae tlie 321
KNOWLTON, F. H., quoted on the flora
Ok the Raton elds ace. sae ee Gee 604
; Some interesting new plants from
Rlorissant, Colorado. es 5 vere ca 88
KoyuKUK-KoBuk region, Alaska... 563-566
Kraus, E. H., elected member of Audit-
ings COMMITHGE... Aeese ce oe Oe
—; Variation of the optic angle of
gypsum with temperature...... 37, 726
KUMMEL, H. B., Stratigraphic study of
the Appalachian and Central States
with reference to the occurrence of
oil and gas discussed by.........
PUISSOU LY a Ads e) atta eau cne eevee aah 49, 741
8, 745
LAKE-SHORE deposits, Effect of rapid
offshore deepening on.......... 50, 746
land district, Foster and
~ Whitney report on geology Ol. waite 317
LAND forms, Technical explanatory
ENGALIMOM SS, Obic, oe ciate tei ow, ate tis Goan 103
LANE, A. C.; Dark scale of hardness.
37, 725
: Demonstration of relative refrac-
tion Ae: Tse GA eal Sie see inane tee ta 37, 125
by 38,
—, Stability of the Atlantic coast dis-
cussed | a oe eRe oer Te it me Ae 49, 741
“LARAMIE” formation (?), Colorado and
NGF IesICO 8 215). Fac beta tare ern et interes 607
LAVA flows, Region of Toyalané and Lu- A
7
— province, British East Africa, The.. 304
LAWSON, ANDREW C., elected Chairman i
Cordilleran Section acs: su Tatra datet ota Tekan 70
-Fanglomerate, a detrital rock at
Battle Mountain, Nevada.........
—. Gedlogy of Steep Rock Lake by. 36, 722
We Geology of the Nevada Hills...... 74
a . Miocene of the southern Coast Range
region of California discussed by. 72
—, Nomenclature of Faults discussed .
BY VS ol wierele tibial eae aed 74
—, Orthoclase as a vein mineral dis-
GusseGs DY ses avant * ‘ 3 heh ane t
— quoted on Nicaraguan Tertiary rocks
; 509-514
—;Section of the Shinarump.......-- 74
754
Page
LEAVES collected from the Dawson ar-
KOS, SuiSE OL ooo cee etere « oxeinl ats cieieas Dhe
LEE, W. T.: Correlation of rocks in the
isolated coal fields around the
southern end of the Rocky Moun-
tains in New Mexico...... 36, 571-686
—, Fossiliferous conglomerates discussed
DWiendverete ere Sue aire epee en wige Se nck 3c 2) ee eee
LEVERETT, FRANK, Discussion of Ne-
braskan and Kansan drifts by.. 45, 735
—; Glacial investigations in Minnesota
dra, BOT wae ieees clas ete we ete eee 46, 732
—, Pleistocene formations and “loess”
adiscussed | bys. cfa4. ce oe eee 48, 739
—, Post-Glacial erosion and oxidation
WISCUSSEG Dye Sb... Gas biome 47, 738
LEWIS, J. VoLNEyY; Paragenesis of the
FENRERT oe Ba oe obs (2k
LEWIS shale, Colorado and New Mexico. 607
LIMESTONE of Steep Rock series, Fos-
SUS POP WOWER? tec. oo re ea Os 46, 123
LIMESTONES, Physical conditions under
which organic and chemically pre-
cipitated are formed {25} eee ee 82
LOESS, a lithological term; B. Se
738
LOGAN, Sir WILLIAM E.; Geology of
Canada, 1868, Reference to....... 371
LOUDERBACK, GEORGE D., Discussion on
fanslomerate Wy. ee cide cease a eee (oe
—elected Secretary Cordilleran Sec-
IOWA Se Bree rA eh oc oa e a < Moe eae ees 70
—, Origin of sandstone near Carson
City; discussed -byiccs 4s es eee oe TZ
—, Orthoclase as a vein mineral dis-
GuSSCG o DY 0 aio Son cess en ew hs eee ee i?
—y;Some general features of the Mio-
cene of the southern Coast Range
recion Of ,CaNioOrnid.. shoe eee eee f (Pe
LULL, R. S.:; Cretaceous Dinosaurs. 85, 208
—, Remarkable skeleton of Stegosaurus .
GISCUSSEGN Dy «Ceo c loko aera ce ate Sota wrereh «aes
Parks, W. A.; A new Trenton crinoid
Prom, Ontario. - casc o fe )\a.08.5 scietee ee
~~, Oriskany sandstones of Ontario dis-
GUSSeCG "DV yo os coe n Solehare eckieieten aie
PENEPLANATION of the plateau, British
WiASt PATDICH ic os laporce yal vhe iene ue canta ore 307
PerissopactyLa, Classification of...... 179
2S ape Ve GAG ye a fae tis css ve aloes ln 85, 179
PERONOPORA, Development of.......... 361
PETERSON, O. A.; Artiodactyla..... 86, 162
PETROGRAPHIC- MICROSCOPIC work, Gran-
RUSTEG YS LIN ore oar teeie chs alata tare te teuel ot, (26
PETROLEUM associated with faults and
dikes, Occurrence of.......... 51, 728
9
PHOTOGRAPHS, Report of Committee on. 35
PHOTOGRAPHY (color), Application to
optica mineralogy of..........-.
PHRASES, The expansion into their full
meaning of condensed............
PHYLLOPORINA CORTICOSA, Development _
PHYSIOGRAPHY of the East African
plateau ; George Lucius Collie.....
PLAINS and valleys, Eastern Washing-
POT os Fae cl eee eye ten alate a ticoda 533
PLANTS from Florissant, Colorado, Some
IN tereNtine 4 HOW ie cs 6. etnies e eieiede es alee
PLATEAU of British East Africa ; George
Euclus ‘Collie: a. < oe into ae 297-316
— plain of Toyalané and Lucero, Domi-
nant Features OP Ss sive ciatcneide-e cae 713
PLEISTOCENE deposits, Perplexity of in-
TOQUE Le SULACR. cise a.ers & wwe eee 709
— formations, Intermingling of........
709-712, 738
—-of Sioux Falls, South Dakota, and
VICINICY: 5 oa HEME R . wc etarccucat= 125-154
PLEURACANTHID®, Cranium of the..... 87
POWELL, Magor J. W., Secretary in-
structed to transmit resolution to
the Secretary of the Interior ap-
proving naming a national park on
the Grand Canyon of the Colorado
BELGE. vine wale wiiie ae fe Gdaaad'e
706
Page
POWELL Nationa] Park, Resolution con-
cerning ‘the naming of’... :... 2026 45
“_ Park of the Grand Canyon,’’ Name
recommended by committee and ap-
Denes by a resolution of the Soci-
QUES -deselere hiede Xo Sa tlabnusiocteets Sidiahs
POST-CRETACEOUS
PraAsopora, Development of........... 3
PRE-CAMBRIAN formations in south-cen-
tral British Columbia; Reginald A.
Day ss ae. owe sees eden eee nee SG, tau.
PRE-CRETACEOUS Dinosaurs; W. J. Hol_
land) a: oo os Conic eee eae eerie 85, 204
PRE-GLACIAL geology of the Puget Sound
Jue INOS OTA 4 Sono Oe col
—— Miami and Kentucky rivers; N. M.
HMenneman< iy si sew are sities 51, 736
PRE-WISCONSIN channels in southeast-
ern South Dakota and northeast-
ern Nebraska; J. E. Todd.. 46, 463-470
— glacial drift in the region of Glacier
Park, Montana; William C. Alden.
44, 687-708
PROCEEDINGS of the Third Annual Meet-
ing of the Paleontological Society,
held at Washington, D. C., Decem-
ber 28, 29, and 30, 1911; R. S.
Bassler’ iS€cretany asa sens che sister
—— — Twelfth Annual Meeting of the
Cordilleran Section of the Geologi-
eal Society of America, held at
Berkeley, California, March 31 and
April 1, 1911; G..D. Louderback,
Secretary wc: hus ee es ae 69-76
— — -—T'wenty-fourth Annual Meeting
of the Geological Society of Amer-
ica, held at Washington, D. C., De-
cember 27, 28, 29, and 380, 1911;
E10: Hovey. Secretany.— es. <--1-% 1-68
Prospect Falls on side of the pre-Gla-
Chal KOTO Nes a ey sere at hey tery evade ree seu 5)
PROSSER, CHARLES S., Resolution of
(HOPG sto) pee eices esis NSE MAG arene ra tare a:
Price® sandstone, Mississippian delta of
Aihere rut Wwe aio phd es ssc GePeyeac oo ore
PRIMATES, Marsupials, and_ Insecti-
vores; W. K. Gregory....... 86, 187
ee Willi arn et BG RCSOLY, alan ivare eels e) oben 194
Pucet Sound basin, Notes on the pre-
Glacial geology of the...........
PULASKI shale, Mississippian delta of
WASTING seis, iS eie vas fonda ene tala aie
Purpun, A. H., Arkansas diamond-bear-
ing peridotite area discussed by. 37, 726
—elected chairman session of Satur-
day, December 30, 1911..........
QUARTZITH, Cataldo... ......22-2+-2-08
Raton section, New Mexico, Correlation
CULE? CLO cys coc) crecie ering fede Abana tele 610
RAYMOND, P. E., De Lorme D. Cairnes
IM LPOCUCCOL Ve eo cutee nies eel tei ean 48
Rep Beps (eastern Oklahoma), Origin
of the sediments and coloring mat-
ter’ Of 2 Js IW. BCCUG. ie plese acon 36, 723
Reeps. C. A., Fossiliferous conglomer-
ates GISCUSSEG DY... = . hele ae
RICHARDSON, GEORGE B.; Monument
Creek group and its relations to
the Denver and Arapahoe forma-
IONS 6 we ee ee ee 36, 267, 276
RiFrt Valley, British East Africa, The.. 312
Riees, E. S.; Notes and slides of the
Uinta: Basin: Hocene: . >... eee 88
RoDENTIA; W. D. Matthew...... ‘aces eke 184
RoGers, AUSTIN F., Discussion on fan-
glomerate DY... .%. >.< -'= san ate eee fe
—: Orthoclase as a vein mineral...... 72
RUEDEMANN, RupDOLPH, Fossiliferous
conglomerates discussed by.......-
—, The Dictyonemas of New Brunswick
discussed Dy. = 2: <5. = 3 = ene
RUSSELL, I. C., quoted on “frock decay.” 539
SAINT PeTER sandstone, C. P. Berkey
i quoted on origin of.............-- 437
SALISBURY, R. D.; Glacial work in the
western mountains in 1901, Refer-
CENCE tO. acs oe.0 sd 6 ee 706
SauLr beds of Seneca Lake............-.- 481
SANDSTONE at the State prison near
Carson City, Nevada, Origin of the. 73
—in New Mexico and Colorado, Da-
KOtR sc cece 66 ote were. © sets) ence aee nnn
SANDSTONES in deltas, Stratification of. 427
—of Ontario, Oriskany........ 83, 371-375
SAN JUAN Mountains of Colorado, Gla-
cial epochs in.). . .- cise 46, 732
SAPONITE, thalite, greenalite, and green-
stone: N. H. Winchell..... 51, 329-331
SAUROPODA: R. S. Gull...) S-peeereee 209
ScaALeE of hardness (dark); Alfred C.
Liane’... c<)es Giese ante oe 37, 725
ScreNcES, Classification of the........ 97
Scorr, W. B., African mammals dis- G
cussed Dy. <. «i«¢ <= =< = sce 85
—, Marine mammals discussed by...-.-.- 85
—, Mesozoic and Cenozoic fishes dis-
cussed DY... s t
SINCLAER, W. J.; Contributions to geo-
logic theory and method...... . 86, 262
= ss lh Ch CT
A el ey
INDEX TO VOLUME 23 757
Page
Sincuair, W. J., Correlation and paleo-
geography discussed by........... 85
—;Some Glacial deposits east of Cody,
Wyoming and their relation to the
Pleistocene erosional history of the
Rocky Mountain region........ pO ar gi
S1oux FALLs and vicinity, Bluff sec-
BRON Ree ee eae arte tol «! cacy'sfe’ sires: oe 136- 144
oe --—, Lerrace or bench sections. .
— — — —, Topography of............
wn section, Pleistocene formation of |
1!
— — — —, ’ Table OL GlEVATIONS.\ 4.05. ite
1
1
Sk1ou, Invention and explanation ‘of
SMITH, PHILIP S.; Glaciation in north-
Rear, AUASKS ow 6 os kc be 44, 563-570
SMitTH, W. S. TANGIER, elected Coun-
ellor Cordilleran Section......... 70_
—; Origin of the sandstone at the State
‘prison near Carson City, Nevada... 73
—, Orthoclase as a vein mineral dis-
CETILSISURTEL TNE ao og
SoutH American mammals; W.B. Scott. 85
sSouTH DaKkora, Pleistocene of Sioux
Hips an) VICINITY... ons. we 125-154
SPENCER, J. W., Closing phase of gla-
ciation in New York discussed by.
sere
; Covey Hill revisited... 36, 471-475, T-
—, —’ Discussion of Nebraskan and Kan-
SLOT CUSTRAR ee rr 47
—j; Hanging valleys and their pre-Gla-
cial equivalents in New York.....
47, 477-485
—, Post-Glacial erosion and oxidation
HS DS S1S0 ol 0 arr 47, 739
—, Stability of the Atlantic coast dis-
WESSEL 0 ee nn em 49. (Al
Spurr, J. E.; Investigation of the Me-
Sool OPES eee ener oe
STANLEY-BROWN, JOSEPH, elected Editor
Geological Society for 1912.......
STANTON. T. W.; Age of Yukon-Alaska
See a ae Pe etree te AS coe ye AS at baie ete 337
—; Fossiliferous conglomerates’ dis-
PURSE en) ty ce Bes sak had eyo. dl oh et 83
— quoted on Mancos and Mesaverde
METIS PME el Sik ciie's oh seco Cee ee aie ey ehes 598
STAUFFER, CLINTON R.; Oriskany sand-
Brones tor (Ontario. ......5.. 83, ofl-aiD
Streep Rock Lake, Geology of; Andrew
0. LUD ee ere 36; 722
— —series, Fossils of lower limestone
to) Ca One le ee e 46, 723
SEERA K.S. Lull... .4.7....h.. 211
STEGOSAURUS, Remarkable skeleton of.. 87
STEPHENSON, L. W., Reference to state-
ment made on coastal ee investi-
PORIDSTEPEREDY Cha ais fot ( e'=],c5m o) ale Mave ad sacs 82
Stosp, G. W., Delta deposits ieee aad
< (
Cie. oe (ew bw aise as « ew eS oo ye « 9 eo
Pie eb a @ 6 6 « ¥ 4 wee « «16 ee se 6 sree eo
by
STRATIGRAPHIC study of the Appala-
chians and central States with ref-
erence to the occurrence of oil and — _
gas; George H. Ashley........ ST. 725
STRATIGRAPHY of the coal fields of
northern central New Mexico; Wil-
RDS) ie ukahes sh gads & aoe" 571-686
Surss, Epwuarp. Congratulatory cable-
gram at annual dinner sent to. 47
— Secretary reports letters rec ceived in 4
answer to cablegram to.......... 47
SYLVANIA sandstone, W. H. Sherze is
ee 437
Page
SYMPOSIUM on ten years’ progress in
vertebrate paleontology ; R. 8S. Bass-
Ler, SACLE TALY’. oho ud waktes crane 85, 155-266
Tarr, R. §., quoted on origin of the
Great. Lakes! DASin. 2) )5,s 0 abate 479
— and LAWRENCE MARTIN; Glacial de-
posits of the continental type in
MATS IEE: , Rather o\tiia-tor aitgle, dice dade eatin 44, 729
TATONIC question, Arthur Keith on new
exidemed! in "the. | wi cee csi ee 35, 720
TaybLor, F. B., Closing phase of glacia-.
tion in New York discussed by.. 47
; Recent studies of the moraines of
Ontario and western New York. 46
TEMPERATURES in the United States,
List of underground
P.O > aes a0 8 6a oie
TENNESSEE (east), Onyx deposits in. 37, 739
TERM, An experiment in the invention’
EG sew aie Je ape anaes Rae ana any bee 115
TERMS over phrases, The advantage of. 112
THRTIARIES, Correlation of American. 234
TERTIARY and later formations, New
Mexiconand Colorado uci jal avie ele 607
aternary geology (some) of
western Montana, northern Idaho,
and eastern Washington; Oscar H.
PVT SIT Gy seb ones cre are: hg meee 75, 517-535
— deposits in the Pacific coast and .
basin regions of North America,
Correlation jof thes cls .cueeow oe 74
2 ——OLsOahw : C. Hi. Hiteheock. 2. 6. (ai
— faunas of the John Day region, Ref-
QEOMEQU TON, 5 iaa,d 28a Oana ate oe a eae 535
— (the middle American), State of our
Knewiedee: fis ccc glettys big a at eioe
PR URGRGE As: Fe. S., Tail <> deravccd uiwenhees 208
Topp, J. E.; Pre-Wisconsin channels in
southeastern South Dakota and
northeastern Nebraska.. 46, 463-470
;South Dakota Geological Survey,
FVETETEMGe: | TOs sees. Skt aces dose
Pena Nevada, Mineral associations
A bape Fores and Lucero: their structure
and relations to other plateau
plains of the desert; Charles R.
ISGVOS Ge erature Ore Anger ac 50, 713-718
eres) LAO CAD LOMA GL airs cei areloiaite. alkene xt Goat kuere 715
TRUE, F. W.; Marine mammals.... 85, 197
TYRRELL, J. B., Glacial investigations in
Minnesota in 1911 discussed by. 46, 733
UInTA Basin Eocene, Notes and slides of
TERE fae Se She NSO eae a eR cehe ic naruue
Utricu, E. O., quoted on Caney Ere
of OKA oOmas sik is aera ehs 458, 459
—, The Medina of Ontario discussed by. 83
; The Ozearieiamn thane. as eittec eee ek 84
Units of geological classification, Sug-
gestions as to definitions of terms
used in designating.............. 12
UPHAM, WARREN, Glacial investigations
in Minnesota in 1911 discussed by.
46, 734
VALLEYS and plains, Bastern Washing-
TOTS gS whan yeuotasetibreia ssa Beararas ava. che eet ale 533
VAN Horn, F. R., Paragenesis of the
Zeolites discussed by.......... 38, 727
VAUGHAN, T. WAYLAND: Coastal plain
investigations conducted by the
United -States and State Geological
SUP VERA. € ait oeWik a dietohchein ke ereiena one Zz
—, D. F. MacDonald introduced by.... 82
—, Geological section Isthmus of Pan-
Bs. CUSGUSREO. Uw sievaielc sy pecs katte 82
758
BULLETIN
Page
VAUGHAN, T. WAYLAND; Physical condi-
tions under which organic and
chemically precipitated limestones
STE. LOrMed. Soll esas oe ae 82
VERTEBRATE paleontologists, Formations
named and described by.......... 262
-—— paleontology, Symposium on the ten
years’ progress in. 32s OD, 2oa-260
VERTEBRATES of the Pleistocene, Estab-
lishment of faunal divisions among :
Ue? 2) 2. eo es ee ee a eso Seeeer aes 7
48, 447-455, 743
VoLCANOES of Hawaii, Succession in :
AEE OV LDE ofc. che oe ala re es 747
WaALcoTT, CHARLES D.; Fossils of lower
limestone of Steep Rock series. 46, 723
= IS We “True introduced Dy¥a= 2<.. +. 85
—:Middle Cambrian crustaceans from
British Columbias 2/35 2 Wace sis s 6 84
—, Secretary Smithsonian Institution,
Paleontological Society welcomed by.
—. The Ozarkian fauna discussed by..
—, W. H: Houmes; and H.C. RizER,
Committee on Powell National
Pea at IS ee ares sy inte ew chet fe 45
WASHINGTON, Henry S.: Suggestion for
mineral nomenclature......... 51, 729
—, Plains and valleys of eastern...... 533
WATKINS GLEN and its pre-Glacial
GQUIVAIORE So [ose antes oe So to ies 483
WrLh Tecords, Ontario -5. -- ss. oe - = 375
WEAVER, CHARLES E.; Notes on the
pre-Glacial geology of the Puget
Sound + Dbasin ss. 6. ase ke os oie ee ee 75
WEBER, MAX, Reference to ‘“‘Die Sauge-
TERE” ZDOOKS TL GES a. as) cs ae Me Ssh ee 187
Wuerry, E. T., Delta deposits discussed
UNS i Ly Sie eho they ONS Sac ee 48, 745
WueETSTONE Gulf and its pre-Glacial
VEL RER Yas cote te sane scecunl reeua tence ciel a Pele 484
WESTGATE, L. G., and E. B. BRANSON;
Cenezoic history of the Wind River
Mountains, Wyoming........-.- 49, 739
WuHItTr, Davip: Characters of Cala-
mites inornatus Dawson.......... 88
—. Correlation of Paleozoic faunas dis-
CUSSEGE PV one - sens Sarees She cn atane 83
—. Delta deposits discussed by..... 48, 744
-— elected Second Vice- President Geo-
logical Society for 1912.......... 2
- Resins in Paleozoic coals...... 37, T28
Wuirtr, ISRAEL C., Discussion of origin
of sediments and coloring matter
of the eastern Oklahoma Red Beds
D¥i. occ tk ate Reeiee'S Gee ee 36, 724
——elected First Vice-President Geologi-
. Cal Society Lom Lees ova. < woke woe os 2
OF THE GEOLOGICAL SOCIETY OF AMERICA
Page
WHITNEY, J. D.; Report on iron ore of
Lake Superior region............ 317
WHITTLESEY, CHARLES; Iron ores of
Lake Superior result of segregation. 320
WILKIE, , of Palo Alto, California,
Tourmalines, benitoites, etcetera,
exhibited . by... < .:. 3 2.0. ass See
WILLIAMS, H. S.; Correlation of the
Paleozoic faunas of the Eastport
Quadrangle, Maine........ 83, 349-352
—, Paleontology of a voracious appe-
tite discussed by... .2.. =. esse e eee 83
WILLIS, BaILEy, quoted on the “Stra-
tigraphy and_ structure of the
Lewis and ivine ranges’’..... 690
WiLuiston, S. W.:; Evolutionary evi-
Gene... 6 as kes ee eee 86, 257
WINCHELL, A. N., J. Howard Mathews
introduced by aed os a eee 5
—. Memoir of Auguste Michel-Lévy by. 32
— — — Christopher Webber Hall by... 28
—: Progress of opinion as to the origin
of the iron ores of the Lake Supe-
bior’ Tevian=......— =o eee 1, 317-324
— +tSaponite, thalite, greenalite, and
ereenstone.. . . - Sonu see 1, 329-332
WiNpD River Mountains, Wyoming, kee
zoic history of. +. 122s eee 739
WiNpb-scour, Arid region of the South,
WeSES. 2 oo. cua cee eee 717
WISCONSIN drift and loess, Des Moines
section. .: : os kc 5. 0. st eee Gb
WoopwortH, J. B.; Boulder beds of the
Caney shale at Talihina, Oklahoma.
50, 457-462
-—, Coastal marshes south of Cape Cod
discussed by. ; . ...--.=. see 50, 742
—, Covey Hill revisited discussed by. 36, 722
—, Structure of the Helderberg Front
discussed by. .. .o..-.. =o 50, T47
WRIGHT, FRED. E. sranularity limits
in oeasra phat. microscopic work.
37, 726
WRIGHT, GEORGE FREDERICK, Pleisto-
eene formations and “loess” dis-
cussed) by. 2]. < ~= oe oan Sees
— ; Post-Glacial and ovxida-
47, 277-296
YUKON-ALASKA geological formations... 334
——_— international boundary, Area we
studies along: .. ... “c.<.s eee ~« bot
— plateau. .....<..~«. ++ = Spee 337
— and Alaska. Differential erosion and
conta in portions of... 333-345
ZEOLITES. Paragenesis of the. 223s 37
ZONES, New Mexico Gastropod, Tres
Hermanos sandstone, Septaria, and
Cephalopod. ......~=<.= o5seeeeee - 595
a De ee
THE GEOLOGICAL SOCIETY OF AMERICA
OFFICERS, 1912
President:
\ HerMAN L. FatrcH Ip, Rochester, N. Y.
Vice-Presidents :
IskAEL C. WHITE, Morgantown, W. Va.
Davip WuitTE, Washington, D. C.
Secretary:
EpMuND Otis Hovey, American Museum of Natural History, New York
City
Treasurer :
Witiram BuLiock CuiarRK, Baltimore, Md.
Editor:
JOSEPH STANLEY-Brown, Coldspring Harbor, Long Island, N. Y.
Inbrarian:
H. P. Cusuine, Cleveland, Ohio
Councillors:
(Term expires 1912)
J. B. WoopwortH, Cambridge, Mass.
C. S. Prosser, Columbus, Ohio
(Term expires 1913)
A. H. Purpug, Fayetteville, Ark.
Hernricu Riss, Ithaca, N. Y.
(Term expires 1914)
SAMUEL W. Bryer, Ames, Iowa
ArTHUR Keitu, Washington, D. C.
‘
tS