, dl at ee
Pein einen <> ms
sect aneene ein ae one
- ue ei — aryntan'
WUT ent Pel cng nent . plienn tata tenes
Aer “ Feed navetnrm int Shatmin
mt spaletane Sorriheatetnactat pete aden Ponrta patch Matehing t

ipemeaie os
een

Pe ahe at Aner:
Peart eA pag wae

ae eth plartebag
f pel oat Age .
om AMenlnenaresanig
St he RADA Bee binclur.
Naieun banasalee ne

LAP Phantom al GNP ym repeata?

Oo Sale a ele,

iota bunct+o Dearne a
pees tds tna
Sebrmtomure cee

He Stary Pm ag -
m GOA Se

gener: 2

PHD, - ae 8 , no eed

GET date ee I neem a ea
9 SA LA Re ee tC PES eee ee = ©

ov = Soa ee ee

HARVARD UNIVERSITY

eh
IS,

LIBRARY

OF THE

MUSEUM OF COMPARATIVE ZOOLOGY

i

POE PP.

i
a

(Wa he hs oe RAL A et

BULLETINS

OF

AMERICAN

PALEONTOLOGY

————__—— Se

VOL. XXVII

a

lIS42 -1943

Babs

Bulletin No.
101.

102.

108.

104,

105.

106.

107.

108.

CONTENTS OF VOLUME XXVIII

New Mollusca from the Pleistocene of San Pedro,
California—II
By S. Stillman Berry

Cephalopods from the Seward pohinente of ieee
By Rousseau H. Flower

An arctic cephalopod faunule from the Vea
of Kentucky
By Rousseau H. Flower ;

Type fossil Cyprzidze of North America
By William Marcus Ingram _

Cephalopods from the Clinton group of New York
By Rousseau H. Flower mae et Ss I
Tertiary and Quaternary fossils “rom the Burica
Peninsula of Panama and Costa Rica
By Axel A. Olsson

A median dorsal plate of eats ae the Tne
Devonian of New York
By John W. Wells -

The Rio Cachiri section in the Sierra de Periia,
Venezuela
By Ralph A. Liddle, Gilbert D. Harris and John
W. Wells - aie
Index S2se0 Ser ee ; RUE 2 Ae one NUL

Plates

14-25

Pages

41- 90

91-122

123-152

153-258

269-368
369

BULLETINS

AMERICAN
PALEONTOLOGY

ye ae nf Compa
Ko Zoology LN

fk a \
' OCT 18 1944

we

VOL. XXVII

ii SSRs SEES ta Le

NUMBER IOI

I94l

PALEONTOLOGICAL RESEARCH INSTITUTION

ItHaca, New York

Ue ea aes

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. a7

No. 102

NEW MOLLUSCA FROM THE PLEISTOCENE

OF SAN PEDRO, CALIFORNIA—II
By

S. Stillman Berry

October 7, rog1

PALEONTOLOGICAL RESEARCH INSTITUTION

ItHaca, New York

ls iS ZA

bie RAe

NE We MOLEUSCA FROM THE PLEISTOCENE OF
SAN PEDRO, CALIFORNIA—II

By

S. STILLMAN BERRY
Redlands, California

This is the second (the first appeared as No. 94A of these Bul-
letins, Berry, 1940) of the preliminary papers incident to my
study of certain Pleistocene biotas of the San Pedro district in
southern California. Diagnoses of seven more species and one sub-
species of mollusks from Hilltop Quarry, believed hitherto unde-
scribed, are here advanced for the consideration and criticism of
other students. All are gastropods, five being members of the
family Turride, which contributes many species and genera to
this fauna and comprises one of its more important and interest-
ing constituent groups. The generic position of most of these
can only be taken as in a high degree provisional, pending the
time when some careful student will undertake far more extensive
investigations of the living animals as well as the shells of this
family than are now anywhere available to us. Until this is done
even the most careful analysis of turrid genera and subgenera can
be little more than tentative, while some forms now placed there
may well prove not to belong to the family at all.

I am deeply indebted to my friend, Mr. Tom Craig, of Los
Angeles, for his kindness in supplying the drawings used in the
accompanying plate, wherein six of the species described are,
we hope, recognizably figured. Illustrations of the two remain-
ing species must unfortunately await a subsequent occasion.

Actzon (Microglyphis) schencki, new species

Diagnosis —Shell small, somewhat barrel-shaped, with a rap-
idly tapering conoid spire; whorls about 5 ; apex smooth, polished,
rounded; later whorls convex, somewhat flattened on the sides,
ornamented by fine growth striations and numerous fine, fairly
sharp, not very regularly spaced, incised, spiral lines, of which

4 BULLETIN 101 4

about 20 can be counted from suture to suture on the penulti-
mate whorl; suture distinct, appressed, but deepening to an ulti-
mately strong shouldering of the whorl in many of the fossils
through the peculiar susceptibility to decortication of this part of
the shell. Aperture broadly auriform; outer lip simple, sharp;
inner lip covered by a well-developed callus continuing past
the pillar to cover the umbilical region; columella in general per-
pendicular, but weakly biarcuate in a greater or less degree and
twisted in front to form a moderately strong fold bordering the
canal, with varying traces of a small secondary fold just poster-
ior to this; canal very short, open, truncate, hardly recurved.

Measurements of holotype.—Alt., 4.9; diam., 3.2; alt. aperture,
3.2 mm.

Holotype.—Cat. No. 10,409, Berry Collection.

Paratypes.—Cat. No. 10,410, Berry Collection; others to be
deposited in the collections of the Paleontological Research In-
stitution, Stanford University, and the United States National
Museum.

Type locality—Lower Pleistocene—‘“Hilltop Quarry” (the
fine-grained upper beds), San Pedro, California; S. S. Berry,
1935-36.

Remarks.—The Microglyphis group of Act@on is poorly rep-
resented in Recent collections, but is not at all rare in the soft,
fine-grained upper layers of Hilltop Quarry. In the somewhat
extended series of shells referable to this subgenus now before
me, in addition to the species just described, I strongly suspect the
presence of a second species of possibly greater frequency, char-
acterized by a sparser spiral striation, strong duplex fold of the
pillar, and a narrow, more strongly curved canal; but decortica-
tion of the shells is so prevalent that only a few of the specimens
are in first-class condition, and it is difficult to be sure how many
of these apparent characters are really critical without a better
knowledge of their normal range of variation. I, hope a little
later to supply figures of both forms, but shall not attempt for-
mally to name the second without a more prolonged study.

Two species from the living fauna alone require comparison
with the fossils. A. (M.) estuarinus Dall (1908a:238) from 92
fathoms, off Estero Bay, California, is materially larger (5 5x3.7
mm.) than schencki, and apparently possesses a relatively lower

5 PLEISTOCENE MoLuLusca oF CAuLir.: BERRY 5

spire (“spire above the last whorl 1.0 mm.”). It seems not to
have been figured. A. (M.) breviculus Dall (1902, p. 512; 1908a,
Pp. 237,238, pl. 15, fig. 12) from 48-53 fathoms, off Santa Rosa Id.,
California, is a thinner-shelled yet stubbier species, with a more
cylindric body whorl and a lower spire than schencki, and only
about half as many spiral striz,

It is a pleasure to associate with this very interesting species
the name of an unfailingly interested and helpful friend, Dr.
Hubert G. Schenck of the Department of Palzontology of Stan-
ford University.

Oenopota turrispira, new species Plate 1, fig. 1

Diagnosis.—Shell small, solid, fusiform, high-spired, with about
8 high-shouldered, narrowly sloping tabulate whorls, which are
almost straight below the shoulder but tend to overhang the deep-
ly cut suture. Embryonic shell mammillate, the first turn, or a
little more, smooth, with rounded whorls, which shortly become
subcarinate and then almost at once develop two strong spiral
cords, the uppermore of which is on the shoulder, while the lower
appears to arise from the peripheral angle, although the suggested
homology is soon obscured by the flattening of the whorls; cross-
ing the spirals and forming strong squarish depressions with and
between them are fine axial threads running across the shoulder
and thence down the outer slope to the lower suture, which short-
ly develop into about 12 massive ribs (strongly retractive on the
shoulder and weakening and narrowing into the suture above)
which increase to about 18 on the body whorl, with interspaces
somewhat narrower than the ribs, and become obsolescent on the
base of the shell approaching the canal; the two spiral threads
previously mentioned after about two turns rather abruptly in-
crease to four and eventually to five intersuturally, and a total
of perhaps 15 on the body whorl, where those nearest the canal.
become indistinct and difficult to count accurately, while in form
they are strongly flattened, with the rather sharply cut grooves
between them hardly half as wide. Underlying the major sculp-
ture is a very fine minor sculpture of microscopic axial threads
and spiral lines visible only under high magnification. Aperture
subperipheral, narrowed, distinctly less than half as long as the
shell; canal rapidly narrowing, moderately long; columella weak-
ly arcuate, flattened, and bounded outwardly by a distinct furrow.

6 BULLETIN 101 6

Measurements of holotype.—Alt., 13.6; diam., 5.5; alt. aperture,
6.1 mm.

Holotype.—Cat. No. 10,400, Berry Collection.

Paratypes.—Cat. No. 10,401, Berry Collection.

Type locality—Lower Pleistocene—‘Hilltop Quarry” (a
shelly pocket in the fine-grained upper beds), San Pedro, Cali-
fornia; I nearly perfect shell and 2 broken spires, S. S. Berry and
ees (Chace; 1926:

Remarks.——This species is large for an CG2nopota and peculiar-
ly high-spired, but exhibits obvious similarities to the Recent fidi-
cula (Gould, 1849, p. 141) described from Puget Sound, and a
nearly allied form has in fact already been reported under that
name from a higher level in the San Pedro Pleistocene. It dif-
fers distinctly from fidicula, however, in the relatively shorter
aperture, narrower form, produced spire, less numerous and
strongly flattened spiral threads, and wide shoulder spiral.

Grant and Gale (1931, p. 514) offer a very elaborate synonym-
ization of the forms of this group, and fidicula is one of the sub-
merged species, but until there has been offered a much more
convincing assembling of evidence for so extreme a view, I find
myself little tempted to follow them. On the contrary it appears
to me quite as likely from present data that a thoroughgoing
analysis will reveal the number of distinct species in this group
to be appreciably larger than is now recognized as that it will
justify so sweeping a recombination. Meanwhile it is surely wise
to move slowly. Even in the works of Sars, who figures the
North Atlantic forms of Ginopota in wide variety, I have been
successful in finding no variant which appears even closely com-
parable to the present form.

The specific name is derived from the L. turris, tower, + spira,
spire.

Moniliopsis chacei, new species Plate 1, fig. 2

Diagnosis.—Shell small, moderately heavy ; spire tall and acute,
with a smooth submammillate nucleus of about 144 deeply su-
tured whorls, which are at first smoothly rounded, later subcari-

Uf PLEISTOCENE Mo.Luusca oF CaALir.: BERRY 7

nate; postnuclear whorls 5+ to nearly 6, at first with a strong-
ly threaded carina, shortly supplemented by a slightly weaker
thread between the carina and the lower suture, and with the
shoulder ornamented by about 16 low axial ridges which form
nodes where they join the carina; on the later whorls these axial
ribs increase in both strength and number to about 23 on the body
whorl, and from the second postembryonic whorl onward they
extend completely across the whorl, fading out only in the region
of the canal, and becoming strongly retractive above the fasciole,
more weakly protractive below it; the early carination diminishes
steadily to the body whorl, the outlines of which are quite
smoothly convex, while at the same time the number of spiral
threads steadily increases both in number and equality of de-
velopment until on the final whorls there are found in addition
to the two major spirals another between them nearly as strong,
a fourth just posterior where the axial ribs make their bend, a
fifth anterior to these which tends to thread the suture, and about
13 or 14 of diminishing strength extending to the canal, besides
often a thread or two just below the suture in the fas-
ciolar area; all these threads save in the region of the canal
are more or less strongly noded where they are intersected by
the axial ribs. Suture of first whorl strongly oblique, subse-
quently normal in character; channeled on the early whorls,
less so on the later ones. Aperture narrow, not quite half so
long as the shell, terminating in a rather long, open, slightly re-
curved canal; outer lip thin, sharp, simple except for the fasciolar
notch, which is imperfect in all my specimens; columella at first
nearly perpendicular, then smoothly arcuate into the canal, with-
out plications.

Measurements.—Largest specimen—alt., 11.5-+; diam., 4.6;
alt. aperture, 5.6 mm. Holotype—alt., 10.1; diam., 3.8; alt. aper-
ture, 4.9 mm.

Holotype.—Cat. No. 10,395, Berry Collection.

Paratypes.—Cat. Nos. 10,396 and 10,399, Berry Collection ;
others to be deposited in the collections of the Paleontological Re-
search Institution, Stanford University, California Institute of
Technology, Pomona College, San Diego Museum of Natural

8 BULLETIN 101 8

History, United States National Museum, and the private collec-
tion of Emery P. Chace.

Type locality—Lower Pleistocene—“Hilltop Quarry” (fine-
eramed upper beds), San Pedro, California +S. S. Beriypekeake
Cross, and i Be Chace, 1934 10.1920:

Remarks.—This characteristic and rather common species in
the horizon studied apparently represents an undescribed race
close to fanchere (Dall, 1903, p. 172; 1919, p. 28, pl. 8, fig. 3),
having the same large nipplelike nucleus but with the sculpture,
especially the axial, of the later whorls notably sparser and coarser
than in either fanchere or rhines (Dall, 1908, p. 248; 1919, p. 28,
pl. 8, fig. 5). It may conceivably lie in the direct ancestral line
of the first-mentioned species. The form and sculpture of the
early whorls as well as the peculiar larval shell strongly suggest
those found in the associated Clathurellas, a circumstance per-
haps more deeply significant than mere coincidence. Both this
species and fanchere differ too strongly in nuclear character from
(e. g.) ophioderma (Dall, 1908, p. 247) to be properly considered
as subspecies or races of the same specific complex.

The species is named for the well-known collector and field-
worker, Mr. Emery P. Chace of San Pedro, who has helped me
greatly in securing abundant material from the Quarry.

Clathurella (Glyphostoma) tridesmia, new species Plate 1, fig.-3

Diagnosis.—Shell small, moderately heavy ; spire tall and acute,
with a smooth submammillate nucleus of a trifle less than two
rounded strongly sutured whorls, the first steeply descending ;
postnuclear whorls 514, at first simply angular at the periphery,
then with a spiral cord developing below the carina, followed
shortly by other spirals and further by the axial sculpture to
take on the character of the mature ornamentation hereinafter
described, Suture of first whorl strongly descending, of subse-
auent whorls normally aligned, appressed, the fasciolar region be-
low it on the later whorls slopingly shouldered and bearing 5 to
6 low, close-set, threaded spirals, with interspaces narrower
than the threads, followed below by a heavier cord just above

9 PLEISTOCENE MOLLUSCA OF CALIF.: BERRY 9

the very heavy nodular band which emphasizes the peripheral
angle ; whorl below the periphery rounded, bearing usually about
20 or 21 strong spiral ribs, the upper ones more or less nodulose,
of which only 3 or 4 remain exposed on the spire, thence on the
last whorl becoming gradually weaker toward the canal; sec-
ond cord below the periphery much larger than its companions,
and sometimes almost as strong as the peripheral cord, forming
a secondary angle to the whorls, though this may vary consider-
ably in strength in different specimens; in a few examples the
next cord, or next cord but one below this, is likewise emphasized
to some extent; threads between the 2 or 3 major cords some-
times reduced to mere intercalaries, at other times as large as
those on the lower part of the whorl. Axial sculpture compris-
ing 17 to 19 (count on penultimate whorl) low, rounded, slight-
ly protractive ribs, which are usually most in evidence on the
spire, becoming nearly obsolete on the anterior part of the body
whorl, and in some specimens so reduced as to be little in evi-
dence save insofar as they produce the previously mentioned
nodulations of the major spirals. Lines of growth inconspicu-
ous. Aperture subovate, with a short, open, slightly recurved
canal, produced at the columella, and a deep rounded anal sul-
cus terminating close to the suture with a strong subsutural cal-
lus; outer lip strongly arcuately produced, somewhat thickened
just back of the sharp, slightly crenulated margin, with usually a
moderately strong varix behind it; apertural denticles wanting
so far as noted; inner lip smooth, sharply sloping at first, but
the rather long columella nearly straight.

Measurements of holotype.—Alt., 10.0; alt. last whorl, 4.6;
diam., 4.0 mm.

Holotype.—Cat. No. 10,393, Berry Collection.

Paratypes.—Cat. No. 10,394, Berry Collection; others to be de-
posited in the collections of the Paleontological Research Institu-
tion, California Institute of Technology, Stanford University,
Pomona College, San Diego Museum of Natural History, United
States National Museum, and the private collection of Emery
iP Chace.

10 BULLETIN 101 10

Type locality—Lower Pleistocene—‘Hilltop Quarry” (pit in
quarry floor), San Pedro, California, (also frequent in the upper
beds)="S.S: Berry, Re 1K. Cross; ands. P. iChace, 1934 to mesa

Remarks.—This is a very beautifully sculptured little species
of a beautiful group, the double angulation of the whorls causing
the spire to appear almost turreted. Grant and Gale (1931) right-
ly bring to question the taxonomic exuberance of Dall, yet it
seems clear that in this as in many other instances they hasten
to the other extreme. Although forms such as the selected holo-
type are very different from anything else in the group known
to me, it is admittedly true that the fossil series is an exceedingly
variable one, so variable indeed that one might well ponder
whether it itself may not include more than one form. Also the
tendency of this variation is very definitely in the direction of
the living cymodoce (Dall, 1919, p. 54, pl. 17, fig. 6), but at no
point does the gap at present seem quite bridged, whether or no
at some later day we find it so. The latter species, as evidenced
by one of Woodworth’s original specimens before me, is very
close to tridesmia, but the smooth nucleus is smaller, the axial
ribs begin almost immediately, they are both more distinctly
knobby and fewer in number, the periphery is much less angular,
especially on the early whorls, the postlabial varix is much
stronger, and the outer lip is both heavier and much less strongly
produced.

C. conradiana (Gabb, 1866, pl. 1, fig. 12; 1869, p. 73) is larger,
with a wider body whorl and much heavier ribbing.

C. canfield: (Dall, 1871, p. 101 ; 1872, pl. 15, fig. 9) is a smaller,
heavier, more strongly ribbed species, with a denticulate aper-
ture and less produced spire.

The specific name chosen is derived from the Gr. tri-, thrice,
-+- desmios, bound, and has reference to the triplicate major
spiral sculpture.

Mitromorpha barbarensis woodfordi, new subspecies Plate 1, fig. 4

Diagnosis.—Shell large for the genus, spindle-shaped, biconic ;
whorls convex; suture channeled, a slender thread visible in the

all PLEISTOCENE MoLuusca oF CALIF.: BERRY il

channel; heavily sculptured with a series of very even, flattened,
spiral cords, about 4 to a whorl between the sutures, and 17 on
the body whorl, their interspaces generally about equal to them
in width, but rather wider at the summit and narrower at the
base of the whorl, the uppermost channel especially wide; axial
sculpture wanting on the final whorl, but on the earlier postnu-
clear turns represented by about 12 low, but quite massive and
narrowly spaced ridges. Aperture narrow, elongate, a little less
than half as long as the shell; columella sinuous, biarcuate, the
columellar folds two in number, but low and usually quite obso-
lete or perhaps immersed in most of the specimens examined;
anterior canal moderately defined and at maturity slightly re-
curved.

Measurements of holotype.—Alt., 11.4; diam., 4.2; alt. aper-
ture, 5.6 mm. “

Holotype.-—Cat. No. 7705, Berry Collection.

Paratypes (all smaller than the holotype or immature) .—Cat.
No. 7706, Berry Collection; others to be deposited in the collec-
tions of Stanford University, the Paleontological Research Insti-
tution, Pomona College, California Institute of Technology, San
Diego Museum of Natural History, and the United States Na-
tional Museum.

Type locality—Lower Pleistocene—“Hilltop Quarry” (pit in
quarry floor), San Pedro, California; S. S. Berry,. R. K. Cross,
aude P Chace 1934 to 1930:

Remarks.—The closest affinity of this, by far the largest mem-
ber of the genus yet to be described, is clearly with M. barbar-
ensis Arnold (1907, p. 438, 446, pl. 57, fig. 1; cf. also topotypes
from Bathhouse Cliff, Santa Barbara, California, in Berry Coll.,
Cat. No. 8958), but it is very much larger, narrower, with a
more produced spire, and the axial ribbing becomes nearly or
quite obsolete on the final whorl at maturity. One of my imma-
ture shells would quite resemble Arnold’s figure were it not for
the heavier and wider axial ribs and their smaller number.
It is the difficulty encountered in the separation of such speci-
mens which lead me for the present at least to withhold full specif-
ic rank from woodfordi, Compared with gracilior “Hemphill”
(Tryon, 1884, p. 317, pl. 25, fig. 62) the pres2nt form differs in

12 BULLETIN 101 12

its much larger size, more produced spire, fewer and coarser
axial ribs, convex whorls, and deeper suture. J/uterfossa (Car-
penter, 1856, p. 429) is interpreted by Grant and Gale (1931, p.
598) to include barbarensis, but I have seen on specimens from
Neah Bay (the type locality) or its vicinity, and can not presume
as to the correctness of their interpretation. Certainly no other
Recent shells of the genus seen by me check at all closely with
the fossils.

Grant and Gale find interfossa (-++-barbarensis) uncomfort-
ably near to aspera (Carpenter), but I fail to understand why
they prefer comparison with this species rather than with gract-
lior. Recent specimens from San Pedro which I can not separ-
ate from gracilior are really very close to Arnold’s figure above
cited, although, on the other hand, they seem clearly distinct
from the Hilltop Quarfy race. Compare also Arnold, 1903 p.
222, ple 4, fie. 10.

The name proposed is in salutation to Prof. A. O. Woodford
of the Department of Geology, Pomona College, and denominates
an exceedingly beautiful little shell, the finest of its group.

Mitromerpha galeana, new species
Diagnosis.—Shell small, spindle-shaped, biconic ; whorls weak-

ly convex, the suture channeled, with a slender thread visible in
the channel; heavily sculptured by a series of even spiral cords,
numbering 5 between sutures on the spire, and a total of about
18 on the final whorl, separated by smoothly grooved channels
narrower than the cords; axial sculpture wanting; aperture nar-
row, elongate, about half as long as the shell; columella sinuous,
biarcuate, bearing two weak folds just below the center; anterior
canal weakly defined.

Measurements of holotype.—Alt., 7.3; maj. diam., 3.3 mm.

Holotype.—Cat. No. 10,397, Berry Collection.

Paratypes.—Cat. No. 10,398, Berry Collection; others to be
deposited in the collections of the Paleontological Research In-
stitution, Stanford University, Pomona College, California Insti-
tute of Technology, San Diego Museum of Natural History, and
the private collection of Emery P. Chace.

Type locality—Lower Pleistocene—‘Hilltop Quarry” (pit in

13 PLEISTOCENE MoLuusca OF CALIF.: BERRY 13

quarry floor) San Pedro California; S. S. Berry, R..K. Cross, and
Be PoChace; 1934) todo 30.

Remarks.—This species stands near filosa Carpenter (1864. p.
658; 1865a, p. 182), but is more slender, the aperture is shorter,
the suture is conspicuously threaded and channeled, and _ the
relative proportions are different, lacking the curious hunched
appearance which is peculiarly characteristic of filosa. Likewise
none of the specimens I have examined show any denticulation
of the outer lip or even the thickening and beveling off seen in
the lip of the latter species.

The species is named for Dr. Hoyt Rodney Gale, to whom,
for his part in the monumental monograph already cited repeat-
edly in this paper, every student, and particularly an isolated

student like myself, must ever remain indebted.
Margarites (Lirularia) aresta, new species Plate 1, fig. 5

Diagnosis.—Shell small, thin, conic, rather high; whorls 51%,
rounded, strongly bicarinate, the carinz acutely threaded, one
carina on the shoulder, the other about equal to it and peripheral,
entering the suture’; slope of shoulder strong, weakly arcuate;
slope between carinze nearly vertical; base typically ornamented
by three spiral cords, the lowest of which strongly angulates the
umbilical margin, with usually an additional lesser cord enclosed
within it; axial sculpture wanting except for the fine but quite
sharp growth lines. Embryonic shell mammillate, at first round-
ed and sculptureless as far as can be made out, but becoming
shouldered after the last turn. Umbilicus open and of moderate
width, well reamed out. Aperture rounded but angulated to
some extent by the carinz; lip thin, sharply beveled, simple, un-
reflected.

Measurements of holotype.—Alt.,4.7 ; diam., 4.4 ; alt. aper-
ture, 2.9 mm.

Holotype.—Cat. No. 10,402, Berry Collection.

Paratypes.—Cat. No. 10,403, Berry Collection; others to be
deposited in the collections of the Paleontological Research In-

1 In some specimens a third weaker carina develops about midway of
the shoulder, but this is more often represented by a mere thread or en-
tirely obsolete. In the holotype there is a minor supplemental keel so
closely subtending the peripheral one as to give almost the appearance of

a single wide riblet in this region; it requires careful inspection to dis-
cover that the apparent rib is mostly an interspace.

14 BULLETIN 101 14

stitution, Stanford University, United States National Museum,
San Diego Museum of Natural History, and the private collec-
tion of Emery P. Chace.

Type locahty—Lower Pleistocene—‘Hilltop Quarry” (from
pit in quarry floor), San Pedro, California; S. S. Berry, 1934,
also Ses. ‘Berry and EP) (Chace, 190377 to! 1930:

Remarks.—l know no species, living or fossil, with which
M. aresta requires special comparison. It is clearly a Lirularia
as that group is at present understood, but even amid this lovely
assemblage its beautiful sculptural plan appears unique. In gen-
eral it somewhat suggests a particularly elegant Valvata. Some
shells show traces of rounded spots of color strung along the
shoulder-carina. Several adult shells were obtained, but the
great majority taken are quite juvenile. Possibly the fragility of
the shell has something to do with this.

The specific name is the L. arestus, pleasing.

Skenea (?) cyclostoma, new species Plate) 1) figs Gna7

Diagnosis.—Shell minute, simple, cyclostomoid; spire de-
pressed, flattened; umbilicus open, widely funiculate; whorls
rounded, rapidly expanding, the suture deeply impressed. Whorls
31%. Aperture almost perfectly circular, large. Sculpture want-
ing except for the very fine and numerous lines of growth.

Measurements of holotype-—Max. diam., 1.76; alt., .g2; alt.
Aperture, -72 man:

Holotype.—Cat. No. 10,407, Berry Collection.

Paratype.—Cat. No. 10,408, Berry Collection.

Type locality—Lower Pleistocene—‘Hilltop Quarry” (fine-
grained upper beds), San Pedro, California; one mature shell,
the holotype, and one minute juvenal, thought to be conspecific
and used as a patatype, Ss. o. Berry, 1037, O40.

Remarks.—I! am by no means sure that this trim and incon-
spicuous vitrinellid is really a Skenea, but its lack of spiral sculp-
ture appears suggestive of this genus rather than of Delphinoidea,
while the well-known S. planorbis Fabricius (Berry Coll. 2286,
taken at Provincetown, Mass., by C. W. Johnson) has seemed

15 PLEISTOCENE MOLLUSCA OF CALIF.: BERRY 15

the nearest thing to it, available to me, for close comparison. From
the latter the present shell differs in (1) the planulate spire; (2)
the lower, much more rapidly expanding whorls; (3) the more
evenly rounded aperture; (4) the finer and less irregular growth
lines ; (5) the smaller initial embryonic whorl; (6) the more pol-
ished surface (especially that of the embryonic whorls) and some-
what thinner shell, even though so alterable a character as tex-
ture is admittedly difficult to use as a basis of comparison be-
tween a fossil and a living shell; and (7) the possession of about
one-quarter whorl less in shells of corresponding size. The dif-
ferences in the embryonic shells as noted may indicate that the
relationship between the two is not so close, but if properly allo-
cated, this is perhaps the first Pacific record for the genus
Skenea.

The specific name proposed has been chosen because of the
marked resemblance in form of shell to the land-operculate genus
Cyclostoma, which in turn derives its name from the Gr. cyclos,
circular, + stoma, mouth, and has reference to the shape of the
aperture.

EV ERATURE. Clik

Arnold, R.
1903. The Paleontology and stratigraphy of the marine Pliocene
and Pleistocene of San Pedro, California, Memoirs California
Academy Sciences, 3, June, 1903, pp. 420, pls. 1-37.
1907. New and characteristic species of fossil mollusks from the
oil-bearing Tertiary formations of Santa Barbara County,
California, Smithsonian Miscellaneous Collections (Quarterly
; Issue), 50 (4), Dec., 1907, pp. 419-447, pls. 50-58.
Berry, S. S.
New Mollusca from the Pleistocene of San Pedro, California
—I, Bulletins American Paleontology, 25 (94A), Sept., 1940,
pp. 1-18, pls. 1-2.
Carpenter, P. P.
1864. A supplementary report on the present state of our knowledge
with regard to the Mollusca of the West Coast of North:
America, Report British Association Advancement Science,
1863. Aug. 1864. pp. 517-686. [Repr. in Smiths. Mise. Coll.,
pp. 1-172, Dec., 1872.]
1865. Diagnoses of new forms of Mollusca from the Vancouver
District, Annals and Magazine Natural History, ser. 3, 14,
Dee., 1864; pp. 423-429; 15, Jan., 1865, pp. 28-32. [Repr.
with preceding in Smiths. Mise. Coll., pp. 233-246, Dec., 1872.]

16 BULLETIN 101 16

1865a Diagnoses of new forms of Mollusca from the West Coast
of North America, first collected by Col. E. Jewett, Annals
and Magazine of Natural History, ser. 3, v. 15, March, 1865,
pp. 177-182 [Repr. with preceding in Smiths, Mise. Coll.,
pp. 277-284, Dee. 1872.]

Dall, W. H.

1871-72. Descriptions of sixty new forms of mollusks from the West
Coast of North America and the North Pacific Ocean,
with notes on others already described, American Journal Con-
chology, 7 (2), Nov., 1871, pp. 93-160; (3), Mar., 1872, pls.
13-16.

1902. Illustrations and descriptions of new, unfigured, or imperfect-
ly known shells, chiefly American, in the U. S. National Mu-
seum, Proceedings United States National Museum, 24 (1264),
1902, pp. 499-566, pls. 27-40.

1908. Diagnoses of new species of mollusks from the Santa Barbara
Channel, California, Proceedings Biological Society Washing-
ton, 16, Dec., 1903, pp. 171-176.

1908. Descriptions of new species of mollusks from the Pacific Coast
of the United States, with notes on other mollusks from the
same region, Proceedings United States National Museum, 34
(1610), June, 1908, pp. 245-257.

1908a. Reports on the dredging operations off the West Coast of Cen-
tral America. . . by the U. S. Fish Commission Steamer ‘‘ Al-
batross’’ . . . XX XVII. Reports on the scientific results of the
expedition to the eastern tropical Pacific . . . by the . . .Al-
batross’’, etc. XIV. The Mollusca and the Brachiopoda, Bulle-
tin Museum Comparative Zoélogy Harvard College, 43 (6),
Oct., 1908, pp. 205-487, pls. 1-22.

1919. Descriptions of new species of mollusks of the family Turri-
tide from the West Coast of America and adjacent regions,
Proceedings United States National Museum, 56 (2288),
1919, pp. 1-86, pls. 1-24.

Gabb, W. M.

1866. Tertiary and invertebrate fossils, Geological Survey of Cali-
fornia, Paleontology, 2 (1), Feb., 1866, pp. 1-38, pls. 1-13.

1869. Cretaceous and Tertiary fossils, Geological Survey of Cali-
fornia, Paleontology, 2, 1869, pp. 1-299, pls. 1-36.

Gould, A. A.

1849. . . . descriptions of . . . species of shells from the collec-
tion of the U. S. Exploring Expedition, Proceedings Boston
Society Natural History, 3, 1849, pp. 140-144.

Grant, U. S. IV, and Gale, H. R.

1931. Catalogue of the marine Pliocene and Pleistocene Mollusca of
California and adjacent regions, etc., Memoirs San Diego So-
ciety Natural History, 1, Nov., 1931, pp. 1-1036, diag. A.-D.
tab. 1-3, text figs. 1-5, pls. 1-32.

Tryon, G. W., Jr.
1884. Manual of Conchology, ser. 1, v. 6, 1884.

Note: Gabb, 1869 and Tryon, 1884 are inaccessible to me, so are cited
perforce from the works of other authors.

PLATE

PLATE 1 (1)

18

BULLETIN 101 18

EXPLANATION OF PLATE I (1)

Figure Page

: Oenopota ‘turrispira,. n.sps -——-—-- ee eee 5

Holotype; alt., 13.6 mm.

. Moniliopsis chacei, n.sp... gE See Rae Ne 6

Holotype; alt., 10.1 mm.

. Clathurella (Glyphostoma) tridesmia, n.sp. 8

Holotype; alt., 10.0 mm.

. Mitromorpha barbarensis woodfordi, n.subsp. 10

Holotype; alt., 11.4 mm.

. Margarites (uirulania)) aresta,, n:Sp.- ee 13

Holotype; alt., 4.7 mm.

> Skenean(2) vey.clostoma, nisp.<=.._ (=. = eee Eee 14

Anterior view of holotype; alt., .92 mm.

. Skenea (?) cyclostoma, n.sp. 1 SAL, 3 14

Basal view of holotype; same scale.

All figures on this page are from original
drawings by Tom Craig

Pu. 1, Vou. 27 BuLL. AMER. PALEONT. Nov l0i Prat

gy
Lay)

<n ~ ot of Commas: 2

Zooire

J

AMERICAN
PALEONTOLOGY

Paleontological Research Institution

Ithaca, New York
Uses a:

J4 3

CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN

PALEONTOLOGY AND PALZARONTOGRAPHICA AMERICANA*

BULLETINS OF AMERICAN PALEONTOLOCY

Volume i, (Nos. 1-5), 354 pp., 82 pls. LM ie ANIM Nie gh ou Tatas Me OSE Cnc} OND
Mainly Tertiary Mollusca,
I¥. (Nos. 6-10). 347 pp., 23 pls. ~ EOS ST GO
Tertiary Mollusca and Foraminifera, Paleozoic faunas.
TH. (Nos. 11-15). 402 pp., 29 pls. 2 Se ae ie
Mainly Tertiary Mollusea and Paleozoic sections and
faunas.
iV. (Nos, 16-21). 161--pp., 26 -pls:° >. =. 5.00

Mainly Tertiary Mollusca and sections of Paleozoic sec-
tions and faunas.
V. (Nos. 22-30). 487 pp., 68 pls. =... SD
Tertiary fossils mainly Santo Domingan, Mesozoic and
Paleozoic fossils,

WES GNO BST) 26S pp OO mpl aes eg ene hay ead an oe fer by 8?)
Claibornian Eocene pelecypods.
Vit. . (No.-32).- 730° pp.,90 pls. = - - betanags Ly 1)
Claibornian Eocene scaphopods, gastropods and cephalo-
pods.
VIET. (Nos. 33-36). 357 pp., 15 pls. _ : Sikes Se haan 5.00
Mainly Tertiary Moliusea.
IX. (Nos. 37-39). 462 pp., 35 pls. Sac Pa ae. T.0
Tertiary Mollusea mainly from Costa Rica.
X. (Nos. 40-42). 382 pp., 54 pls. 8.00

Tertiary forams and mollusks mainly. from ‘Trinidad “arid
Paleozoic fossils.

XI. (Nos. 43-46). 272 pp., 41 pls. cree ene a
Tertiary, Mesozoic and Paleozoic fossils: “mainly from
Venezuela.
XII. (Nos. 47-48), 494 pp., 8 pls. Sis Ss 6.00

Venezuela and Trinidad forams and ‘Mesozoic inverte-
brate bibliography.

XII. (Nos. 49-50). 264 pp., 47 pls. _- 6.00
Venezuelan Tertiary Mollusca and Tertiary Mammalia.
X1V. (Nos. 51-54), 306 pp., 44 pls. ‘ 6.50

Mexican Tertiary forams and Tertiary mollusks 3S of Peru
and Colombia.

* Complete tilles and price list of all numbers mzsy be had on applica-

sion. All volumes available,

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 102

CEPHALOPODS FROM THE SEWARD
PENINSULA OF ALASKA

By

Rousseau H. Flower

December 8, 1941

Paleontological Research Institution

Ithaca, New York
Urs. 2:

ae

of Com =a
; GP restos, “N
DEC 22 i)

LIBRAR®*

1346!

CEPHALOPODS FROM THE SEWARD! PENINSULA
OR ALASKA

by

RoussEAU H. FLOWER

The three species of cephalopods described in the following
pages were collected from the York District, Seward Peninsula,
Alaska, by J. B. Mettie, Jr., of the U. S. Geological Survey. They
were sent to the writer through the kindness of Dr. Josiah
Bridge. The specimens have been of exceptional morphological
interest, but serve only to establish approximate correlations of
the beds from which they came. Two of the species belong to
Ellesmeroceras, a genus known only from the Ozarkian of Amer-
ica and the equivalent Wanwanian of Manchuria. The Alaskan
forms are much closer to the Manchurian forms than to the single
species thus far described from the Western Hemisphere, Elles-
meroceras scheu Foerste. The two species of Ellesmeroceras, col-
lected from float, indicate the presence of Ozarkian strata.

The remaining species, a coiled cephalopod, is Canadian in
aspect. Externally, the form is one which shows no essential dif-
ference from Plectoceras of the Ordovician. The siphuncle, how-
ever, shows a thickening of the connecting ring which is peculiar
to certain Canadian cephalopods, including Tarphyceras and
Eurystomites. It remained to determine whether the external
form or the internal structure was the more significant feature
to be used in classification. Other investigations indicate strongly
that two distinct groups are involved in early Paleozoic coiled
cephalopods. One of these, characterized by a thick connecting
ring of complex structure, is known only from the Canadian. This
includes Tarphyceras and Eurystomites, and it seems desirable to
restrict the Tarphyceratide to such forms. Another group, thus
far known definitely only from the Ordovician, is characterized
by thin connecting rings which show no differentiation of struc-
ture. This group includes Plectoceras of the Plectoceratide and
a number of genera formerly assigned to the Tarphyceratide, in-
cluding Barrandeoceras. Further, Chazyan coiled cephalopods

4 BULLETIN 102 99

externally typical of such Canadian genera as 4 phetoceras, Pyc-
noceras, and probably Falcilituites belong in this group. Unsettled
problems of phylogeny make it impossible to revise the classifica-
tion of the genera involved at the present time. It is conceivable
that a simplification may have taken place in a single genetic line,
producing Ordovician types from Canadian ones. On the other
hand, the internal structure suggests very strongly that, instead,
two lines may be involved which illustrate one of the most re-
markable cases of homeomorphy to be found among the cephalo-
pods. Which of these possibilities contains the true solution can-
Lot be determined until more thorough investigations have been
undertaken. Happily this 1s now being accomplished by Miller
and Furnish, in the completion of the studies of Ozarkian and
Canadian cephalopods.

Genus ELLESMEROCERAS Foerste

Revised description.—( Ulrich and Foerste, 1936, pp. 275-6.)

“Conchs orthoconic, slowly enlarging, laterally compressed.
Sutures of septa curving downward laterally, rising almost as
high dorsally as ventrally, but a little straighter on approaching
the ventral saddles. Closely similar to Ectenolites, but regarded
as orthoconic rather than cyrtoconic.

Siphuncle in flattened contact with one of the more narrowly
rounded sides of the conch; structure probably holochoaniodal.
Differing from Cotteroceras chiefly in the downward curvature of
the septa laterally.

Genotype: Ellesmeroceras scheu Foerste (Denison Univ. Bull.,
Ser, Lab, jou, vol: 19, p. 265, pl 27, fe: 3Aec> pla sae tice
(Gives

The above description differs mainly from the original one,
which is combined with the description of the genotype and is too
long to be reproduced here, in the recognition of dorsal saddles
of sutures. The illustration did not show the dorsal sutures clear-
ly, and no mention of them was made in the original description.
The Alaskan species are atypical mainly in that the dorsal saddle
is better developed than is the ventral saddle. This is, however,
a feature which may be expected to vary among the species. Such

23 ALASKAN CEPHALOPODS: FLOWER 5

sutures are not known in any described orthoconic genus of the
early Paleozoic, though they are characteristic of the genus Ecten-
olites Ulrich and Foerste (1936, p. 272) which possesses trun-
cated endocones within the siphuncle and is slightly cyrtoconic
in the adapical part of the shell. One of the Alaskan species shows
a very slight cyrtoconic tendency, but this appears to be variable
within the species.

The only described species of Ellesmeroceras consist of the
genotype and several forms from the Wanwanian of Manchuria.
The forms discussed in this paper are mest closely allied to Flles-
meroceras foerstei obayashi (1932, p. 268, pl. 1, fies. 1, I1), a
species of rather strongly compressed section and well-developed
lobes, the dorsal saddles of which are quite conspicuous, at least
anteriorly. This species appears to cornect the Alaskan forms
with the genotype, at least insofar as the condition of the sutures
is concerned. Other cescribed Manchurian species are broader in
section and have straighter sutures.

The structure of the siphuncle has not been closely studied in
any species of Ellesmercceras. The siphuncle is made up of con-
cave segments which are oblique, being strongly inclined orad on
the ventral (7) side, where the siphuncle is practically in contact
with the wall of the shell. The concave outline of the seements
seems to be the only basis for classifying the genus as holochoan-
itic. The siphuncle is illustrated adequately in my plates. Ex-
foliated siphuncles, exposed on the ventral side of the conch (PI.
1, figs, 1-2), present the aspect of cyrtochoanitic segments. In
section (Pl. 1, fic 19) this aspect is retained. However, close ex-
amination shows that the septa join the siphuncle at a point orad
of the greatest width of the segment and apicad of the least width
and are not located at the apparent septal foramen at all. Dorsally
(Pl 1, fig. 9; Pl. 2, fig. 6) the segments are concavosiphonate,
but again the septa do not join the siphuncle at the point where
they would normally be expected to be found. Septa were gener-
ally elusive, as were the fine points of the structure of the si-
phuncle wall, because of extensive replacement and recrystalliza-
tion of the white calcite that filled the phragmocone for the most
part. However, one section (PI. 2, fig. 6) showed the course of the
septa clearly and gave in addition good indication of the original

6 Buiietin 102 24

structure of the siphuncle wall. At the base of the specimen, septa
could be seen passing through areas of dark matrix and joining
the siphuncle. The septal necks are bent before attaining the wall
cf the siphuncle itself.

Further, they seem to terminate shortly beyond the bend and
to be discontinuous with the wall of the siphuncle. The nodes
of the siphuncle lie shortly apicad of the bend of the neck. Also,
there is indication that the walls are thickened, being widest api-
cad of the middle and shaped somewhat like a crescent or a
meniscus. The interpretation of the structure of the siphuncle
wall here can be seen by comparing Plate 2, fig. 6 with text figure
1A. Segments lying slightly farther orad in the same specimen
furnished additional evidence of the ellipochoanitic structure.
Here the camere are filled with white calcite and the free part
of the septum is not visible. However, dark calcite lying close to
the siphuncle marks in part the exterior of the siphuncle wall and
preserves the bent portion of the septal necks (text fig. 1B). Ow-
ing to recrystallization of the material, particularly the white cal-

Fig. 1. Internal structure of siphuncle walls of Alaskan cephalopods.

A. Dorsal wall of siphuncle of Ellesmeroceras bridgei, from basal part
of Plate 2, fig. 6. Cavity of siphuncle on right.

B. Showing appearance and restoration (broken lines) of dorsal wall
of EH. bridget farther orad in the same specimen.

C. Siphunele in Plectoceras sewardense, showing differentiation of con-
necting rings. Oblique course of septal foramen indicated by dotted line
across the siphunele.

25 ALASKAN CEPHALOPODS: FLOWER 7

cite, no further structures could be seen in the material. Investi-
gation of the structure by thin section did not seem warranted by
the present condition of all specimens observed and was further
undesirable in view of the small amount of material available for
study.

The thickening of the connecting ring is not a unique feature,
confined to this genus, but is known in a considerable number of
other cephalopod genera, including Bathmoceras, a number of
Canadian genera formerly supposed to be holochoanitic, in-
cluding Protocameroceras and several other forms. The signifi-
cance of this structure will be discussed at another time.

According to Ulrich and Foerste (1936, p. 260): the Holo-
choanites are represented in the Ozarkian by three genera: Elles-
meroceras, Walcottoceras, and Pachendoceras. The present ob-
servations make it necessary to remove Ellesmeroceras from this
list. Other genera have not been examined sufficiently closely to
remove all doubt as to whether the condition may not be identical
with that of Ellesmeroceras.

From the original descriptions, lValcottoceras appears to be
little more than an annulated edition of Ellesmeroceras, while
Pachendoceras is differentiated from it on the basis of its de-
pressed section.'

Certainly the first forms which can be considered as holochoan-
itic beyond all possible doubt are younger than the Ozarkian.
Further, rather desultory observations on supposedly holochoan-
itic Canadian forms have thus far failed to reveal other than
ellipochoanitic structure, suggesting that the oldest of the true
Holochoanites may be Ordovician,

Ellesmeroceras bridgei Flower, n. ssp. Plate 1; Plate 2, fig. 6

Conch straight, compressed, expanding slowly, the height about
3 mm. greater than the width; section compressed with the ven-
tral (?) or siphonal side very slightly more narrowly rounded
than the antisiphonal site. Expansion is gradual. The largest
form observed increases from 14 mm. and 17 mm. to 17 mm. and
20 mm. in the basal 30 mm., and to 21 mm. and 24 mm. in the
next 20 mm. The rate of expansion is uniform in the specimens
observed. The sutures bear lateral lobes which rise to a relatively

1 Pachendoceras apparently possesses true endocones and is therefore

included in the Endoceroidea. While probably ellipochoanitic, it is not
closely related to Ellesmeroceras,

8 BULLETIN 102 26

low and broad ventral saddle, not fully observed because of the
tendency for the wall to break away at this region exposing the
siphuncle. The dorsal saddle is relatively high and narrow.

Camere occur four and a half in 10 mm., where the adoral
shell width is 15 mm.; six probably occuring in a length equal to
the adoral width of the shell over the region measured. The
siphuncle indicates that the camerze become more closely spaced
adorally, eight and a half segments occuring in a length equal to
a width of 20 mm, in another individual.

The siphuncle lies close te the venter: In general, it liesiam
contact with the ventral wall at an earlv stage, later becoming free
and separated from it by a short interval. At a shell height of 19
mm., the siphuncle is faintly depressed in section, measuring 3
mm. by 4 mm. and is in contact with the wall (Pl. 1, fig. 5).
Farther on in the same specimen, where the height is 23 mm.,
the siphuncle is 1 mm. from the venter, essentially circular, with
a diameter of 4 mm. The appearance of the siphuncle segments
as exposed on exfoliated specimens is adequately shown by our
figures and has been discussed, along with the structure of the
siphuncle, in connection with the description of the genus. The
siphuncle is clearly without any internal organic deposit other
than that supplied by the thickening of the connecting rings. Sev-
eral specimens show the adapical portion of the siphuncle filled
with calcite, and often the margin between the calcite and the
matrix is such as to suggest the presence of diaphragms in the
siphuncle. However, comparison of a number of specimens shows
that the form of the contact is variable. In Plate 1, fig. vo the
calcite extends farthest orad on the ventral side. Other specimens
have been observed in which the calcite slopes orad on the dorsum
and even laterally. A laterally inclined contact is shown in cross
section in Plate 1, fig. 5. The variation in orientation seems to be
a clear indication that the contact is merely the junction of matrix
forming an incomplete internal mold within the siphuncle and the
complemental filling of calcite. Kobayashi (1935, p. 22, text fig.
2) has illustrated the Ellesmeroceratidz as holochoanitic and as

7. ALASKAN CEPHALOPODS: FLOWER 9

possessing diaphragms. Our forms are clearly not holochoanitic
and show no trace of organic dissepiments.

The surface of the shell is smooth and is preserved in several
individuals. It is void of striations or any visible lines of growth.
It does, however, show faint color markings which are sufficiently
uniform in several individuals to suggest strongly that they repre-
sent an original color pattern. The markings form lateral lobes
which rise steeply orad on the dorsum, much more steeply than
the sutures, and are nearly transverse on the venter. Similar
markings are also shown on the following species.

Discussion.—The prominence of the dorsal saddles, together
with the slender form of the species and the separation of the
siphuncle from the ventral wall at a shell height of 21 mm., will
serve to distinguish this from all other species. The associated
form differs in having the siphuncle separated from the ventral
wall at a much earlier stage, possibly throughout the entire shell,
and in being a smaller and a relatively rapidly expanding species.

Types.—This species is based upon a series of four syntypes, all
the property of the U. S. Geological Survey, to be deposited in the
U. S. National Museum.

Occurrence.—From the York District, Seward Peninsula, Alas-
ka. All of the specimens are from a single piece of float from the
bed of Cassiterite Creek, about 1.3 miles northeast of Cassiterite
Mine. The beds from which these forms came are presumably
Ozarkian, as the genus is known only from that period,

Ellesmeroceras expansum Flower, n. sp. Plate 2, figs. 3-5

This species is represented in our material by a single speci-
men which differs radically from FE. bridgei in the more rapidly
expanding section, a siphuncle that is separated from the ven-
ter at a much earlier stage, and the relatively narrowly rounded
condition of the venter. The extant portion of the phragmo-

cone has a maximum leneth of 25 mm. and expands from a

2 This conclusion secms to be based on the presence of rather dubious
dissepiments within Sinocremoccras and Multicameroceras which Kobayashi
had formerly placed in the HEllesmeroceratide. He later removed them
properly to the family Plectronoceratide. He occasionally speaks of both
families as ‘‘cllesmeroceroids, ’”

10 BuLLETIN 102 28

height of 12 mm. and a width of g mm. near the base to a
height of 17 mm. and a width of 14 mm., in a length of 20 mm.
At the base the siphuncle is 1 mm. wide, 1.4 mm. in height,
and about .8 mm. from the ventral wall. Adorally the siphuncle
is 2mm. wide, 2.8 mm. high, and 1 mm. from the venter.

The sutures, shown only at the adoral end of the specimen,
have only faint lateral lobes and rise equally on the dorsum
and venter. The depth of the camerz is not noted. The sep-
tum, shown at the adoral end of the specimen, is uniformly
curved.

The lateral surface of the holotype shows color bands similar
to those already mentioned in connection with EF. bridget. Un-
fortunately they are too faint to be illustrated clearly by natural
photographs of the specimen.

Type.—Holotype, U. S. Geological Survey, to be deposited in
the U. S. National Museum.

Occurrence.—Found associated with the above species in
float trom! the “bed! oi Cassiterite Creek, 1.3 mi. northeash on
Cassiterite Mine, York District, Seward Peninsula, Alaska.

Genus PLECTOCERAS Hyatt

Genotype—Nautilus jason Billings.

Plectoceras Hyatt, 1884, Proc. Boston Soe. Nat. Hist., vol. 22, p. 268;
Hyatt, 1894, Amer. Phil. Soc., Proc., vol. 32, p. 499; Miller, S. A., 1897,
North American Geol. Pal.. 2d App. p. 776; Whiteaves, 1906, Geol.
Surv. Canada, Pal. Foss., vol. 3, pt. 4, p. 299; Ruedemann, 1906, New
York State Museum Bull. 90, p. 482; Grabau and Shimer, 1910, North
American Index Fossils, vol. 2, p. 72; Troedsson, 1926, Meddelelser
om Groénland, vol. 71, p. 41; Foerste, 1933, Denisen Univ. Bull., Sei.
Lab. Journ., vol. 28, p. 119; Foerste, 1935, Denison Univ. Bull., Sci.
Lab., Journ., vol. 30, p. 90.

The genotype of Plectoceras is from the Chazyan of the
Mingan Islands, Quebec, but has also been identified from the
Chazyan of the Champlain Pasin, where it is represented by
larger and more abundant specimens. The genus is erected for
costate coiled cephalopods, the cost sloping from the dorsum
to a hyponomic sinus on the venter. The sutures are straight
and transverse or may cevelop lateral lobes, though this does
not apply to the genotype. Foerste has separted the genus
Metaplectoceras (Foerste, 1935, p. 91), which differs mainly
from Plectocercs in the tighter coiling and the development of

an impressed “zone, with Inachus undatus Hall of the Black

29 ALASKAN CEPHALOPODS: FLOWER 11

River limestone of Watertown, New York as the genotype.
Curvature of the genotype of Plectoceras is known to be quite
erratic and variable, with the whorls sometimes free, some-
times in contact, and sometimes so closely appressed that the
dorsum is flattened as much as in Plectoceras occidentale, P.
lowt, and P. halli. For this reason it does not seem advisable to
recognize Metaplectoceras Foerste as a distinct genus. This
leaves, included in Plectoceras, the following species:

Plectoceras jason (Billings), Chazyan, Mingan Islands and
the Champlain Valley.

P. tyrans (Billings), Chazyan, Mingan Islands.

P. undatum (Conrad), Black River limestone, New York
and Ontario.

P. halli (Foord), Black River limestone, New York and
Ontario.

P. carletonense Foerste, Black River limestone, Ottawa
Valley, Ontario.

P. foerstet Troedsson, Cape Calhoun series, Greenland.

P. lowt Foerste, Black River limestone (?) Pt. Burwell,
Labrador.

P. occidentale (Hall), Platteville.

P. landerense (Foerste), Bighorn dolomite.

The siphuncle lies close to the ventral side of the shell. The
septal necks are straight and short, and the connecting rings
are thin and without differentiation of structure. The siphuncle
has been studied in detail by Troedsson for Plectoceras foerstet,
for which he has illustrated the structure in thin section (19206,
pl. 2, fig. 1), and the writer has been able to study well-pre-
served specimens of P. halli (Foord) which shows similar
structure. While material has not been adequate to study the
structure thoroughly in the genotype, such material as was
available indicates that there also the connecting ring is prob-
ably thin and simple.

The specimen described here from the Seward Peninsula of
Alaska differs from Ordovician species of Plectoceras in the
structure of the siphuncle, but the other features of the shell
supply only minor differences which do not seem to be adequate
for setting the species apart in a different genus. The umbilical
perforation is larger than in other species of Plectoceras, and

12 BULLETIN 102 30

the conch seems to expand relatively slowly The exterior is typi-
cal of Plectoceras. The best difference is perhaps supplied in the
course of the sutures, which lack lateral lobes but are inclined
forward on the dorsal side of the shell. Nevertheless all of these
differences are more or less closely approached in one or another
species of typical Ordovician Plectoceras.

The wall of the siphuncle, however, differs in structure, not
only from all known Plectoceras, but from all post-Canadian
cephalopods so far studied in detail. The structure, illustrated in
text figure 1C, consists of very short septal necks, scarcely re-
curved on the doral side, and essentially straight and continuous
with the oblique septum on the venter. The remainder of the seg-
ment is composed of thick connecting rings which are differenti-
ated into an outer light-colored layer and a thin, darker inner
layer. Differentiation of the two layers is clear on the venter, but
rather cbscure on the dorsal side of the siphuncle. This condition
is almost identical with that observed in Eurystomites kellogi cf
the Beekma: town of New York, and is similar to structures found
in related species beth of this genus and of Tarphyceras.*

The study of a number of genera formerly placed in the Tar-
phyceratide indicates that coiled Ordovician cephalopods are
sharply divisible into two groups on the basis of the structure of
the connecting ring. It remains to be determined whether these
two groups are actually related, or whether they only exhibit a
remarkable degree of homeomorphy. To determine this it is nec-
essary that the details of siphuncular structure be studied for all
genera of the Tarphyceratide and Plectoceratidee. Further, it is
eminently desirable that as many species as possible be investi-
sated, particularly for genera which apparently pass from the
Canadian to the Ordovician. It is believed that this matter will
be dealt with very adequately in the study of Ovarkian and Can-
adian cephelopods now being completed by Dr. Miller.

2
3

Ulrich and Foerste (1936) have subdivided these genera, particularly
Tarphyceras, on the basis of section and rate of coiling. The genera are
used here in their older and broader usage. This is partly because the
descriptions now available leave considerable doubt as to the best place to
se’ the hovndarics between te new genera and the old ones as restricted,
end partly because the proposal of these new gerera seems to be a procedure
of doubtful benefit in expressing the relationships between species.

31 ALASKAN CEPHALOPODS: FLOWER ue

The species here referred, with misgivings, to Plectoceras have
been placed there so as not to interfere with the study now in
progress. The structure of the connecting ring shows that it
should properly be placed in the Tarphyceratide, or, if such
separation seems desirable, in a new family related to the Tarphy-
ceratidze but grouped with it and not with the Ordovician forms.
Possibly it will prove to belong to the inadequately known Delto-
ceras or to a genus as yet undescribed.

There are other cases known of a strong resemblance in gross
features between Canadian and Ordovician cephalopods, but there
is not enough information published as yet to determine whether
there is a similar discordance in the structure of the connecting
ring. Barrandeoceras, formerly placed in the Tarphyceratide,
but Ordovician and not Canadian in range, has simple and very
thin connecting rings. In the Chazyan, Trocholites has a siphuncle
of Ordovician aspect. Also, species of the Chazyan, which are
otherwise apparently typical of Aphetoceras and Pycnoceras, pos-
sess simple siphuncles of the type found commonly in the Ordo-
vician. It is not known as yet whether the Canadian genotypes
possess simple or thickened connecting rings. Further, the simple
connecting ring is found in the species described as Tarphyceras
multicameratum Kuedemann of the Chazyan.*

Much more study is necessary to establish the value of these
structures in classification. Certainly there is abundant evidence
of strong superficial resemblance between Canadian and Ordo-
vician coiled cephalopods. Present facts show that Canadian
coiled cephalopods have siphuncles very different from Ordovi-
cian coiled forms, suggesting that two major groups are involved,
with no good evidence at the present time of intergradation
despite the strong external similarity between the two groups.
While it is not unlikely that some forms with simple connecting

4 These species, which are to be described in my long-delayed study of
the Chazyan cephalopods of the Champlain Valley, include some undeseribed
forms. Although curvature is such as to permit these associated forms to
be placed in different genera, it is believed that here is a case in which such
generic definitions have already been carried too far. The species are sim-
ilar in section, exterior, and spacing as well as the course of the sutures.
They differ in no essential respect except the rate of coiling. It is strongly
felt that they represent a single Chazyan genus, though referable to Aphe-
toceras, Pynoceras, Falcilituites, and Tarphyceras on the basis of the extant
deseription of those genera.

14 BuLLETIN 102 32

rings may be found in the Canadian, there is no evidence
as yet to suggest that the complex connecting rings ever pene-
trated the Chazyan, nor is there any reason to believe that the
two groups intergrade.

“Plectoceras” sewardense Flower, n. sp. Plate 2, figs. 1-2

Conch coiled, with the early whorls in contact, the later part
of the last whorl free when mature. The holotype has a maximum
disc of 105 mm. and consists of two and a half preserved volu-
tions. Quite probably about half a volution is missing from the
adapical end. The whorls are circular in section in the early
stages, but the venter becomes flattened in the last whorl and the
greatest width comes to lie close to the ventral surface, the sides
converging from the abdominal to the umbilical shoulders. The
mid-dorsal region has not been cbserved where the whorls are in
contact ; probably it 1s shghtly flattened, as it retains this condition
at the base of the mature living chamber where the whorl is free.
Coiling is not tight enough to produce an impressed zone. Near
the aperture the whorl becomes shghtly compresse1, and the ab-
dominal shoulders become more rounded ant the ventral face
less distinct. The height of the whorl increases more gradually
than in most Plectoceras. The apparent umbilical perforation has
a minimum diameter of 6 mm. The whorl at the base has a height
of 6 mm., which increases at intervals of a half volution to 9 mm.,
16 mm., 23 mm., and 29 mm. In the first volution the width of
the shell lies halfway between the dorsum and the venter, but
it moves ventrad rapidly in the next half volution. The height
and width increase from 17 mm to 20 mm. in the basal fourth of
the last volution in a vertral length of 50 mm. The next half
volution shows an increase of the height to 28 mm., with the
width apparently the same. At the aperture, slightly more than
a quarter of a volution farther, the height is 30 mm., with the
width estimated at between 26 mm. and 28 mm.

The course of the sutures, not shown clearly on the specimen,
is known only from the base of the living chamber. The suture
is without lateral lobes, is essentially straight but inclined strongly
forward from venter to dorsum, the inclination apparently being
about equal to that of the lateral portion of the cost, though less

33 ALASKAN CEPHALOPODS: FLOWER 5

inclined than the coste as they approach the extreme ventral por-
tion. The camerz, of which the last three are preserved on the
paratype, are variable in depth, measuring I mm., 2 mm., and 1.5
mm., progressing orad.

The siphuncle lies in contact with the venter at least in the
last whorl. Its structure is shown in fig. 1C. The connecting rings
present slightly concave vertical outlines. The septal necks are
short, scarcely attaining the cavity of the siphuncle, being overlaid
by the tip of the connecting ring of the next adoral segment. The
connecting rings are relatively thick. On the venter the con-
necting ring is divided into two portions, an inner dark-colored
band, relatively thin, and a thick lighter outer band which occu-
pies all of the space up to the wall of the shell. On the dorsum,
the differentiation between the layers is not so clear. One seg-
ment shows a faint trace of differentiation of the tip of the con-
necting ring, producing the eyelet structure described in another
paper, but it is so obscure that I have not attempted to reproduce
it in the drawing.

The surface of the shell is not clearly preserved in the early
portion, though incipient coste are indicated there. In the last
whorl coste become prominent laterally, strong ventrolaterally,
decreasing in strength gradually as the umbilical shoulder is ap-
proached and disappearing abruptly on the ventral surface. The
coste are inclined apicad from dorsum to venter, and are slightly
curved with the convex side directed orad, the slope increasing
as the venter is approached. About two cost occur in a length
equal to the adoral height of the shell. Near the mature living
chamber the coste are lost internally and are expressed exter-
nally only as thickened lire. Transverse lire mark the entire shell
surface. These follow the course of the coste and continue over
the venter forming a deep rounded hyponomic sinus. The living
chamber, which is complete on the holotype, has a basal height
of 25 mm., taken normal to the shell rather than the oblique sep-
tum, and a ventral length of 85 mm., including about a quarter of
a volution. The shell is free from the base of the living chamber.

16 BULLETIN 102 34

Discussion.—Insofar as the gross features of the shell are con-
cerned, it is relatively simple to distinguish this species {rcm all
that have been described previously. It is distinctive mainly in
its umbilical perforation, which is large in comparison to
Flectoceras species of a comparable size, followed by relatively
slender whorls, gradually expanding, with the width and height
about equal up to the mature living chamber where the whorl be-
comes faintly compressed and the greatest width no longer lies
close to the ventral surface, where it moved in the second whorl.
The Chazyan species of Plectoceras, including the genotype, are
relatively broad in section, the early stages expand very rapidly,
subsequent expansion of the shell is more rapid, and the section
tends to become depressed. Most species can be separated by the
oval section, for even where the venter is flattened, as in P. lowt
Foerste, the greatest width never lies far ventrad of mid-height
of the section. In this respect our species resembles only Plec-
toceras halli (Foord) of the Black River limestone of New York
and Ontario, in which the expansion of the shell is more rapid.
Strangely enough, the species which is closest to this one geo-
graphically, P. foerstei Troedsson (1926, p. 42, pl. 2, fig. 1; pls
11-12). is very different in section, being strongly compressed
from a relatively early stage, with the greatest width consistently
at mid-height of the whorl. A feature in which our species agrees
with the Chazyan genotype and differs from all younver species
is the extreme proximity of the siphuncle to the ventral wall of the
shell. Our species has the siphuncle exposed at two places in the
paratype. In one, at the base of the last whorl, it is apparently
separated from the venter, though this is partially accounted for
by the fact that the section does not penetrate the center of the
shell. On the other section, a quarter of a volution farther, the
siphuncle is close to the venter as described above. The condition
of the siphuncle also recalls the condition found in Deltoceras
vaningent Ruedemann (1906, p. 480, pls. 25-28). Comparison
with typical Deltoceras is not possible because the genotype is in-
adequately described and has never been figured. The Chazyan
species, which is essentially a compressed edition of Plectoceras
with relatively rapid vertical expansion, and which shows costee
similar to those of Plectoceras under favorable conditions of pres-
ervation, is probably most closely related to the smaller Plecto-

35 ALASKAN CEPHALOPODS: FLOWER 7

ceras tyrans (Billings) of the same horizon of the Mingan Islands.

The structure of the wall of the siphuncle indicates that this
Alaskan species is not a Plectoceras. The significance of the
structures has been discussed in connection with the genus and
is here consicered adequate to indicate the Canadian age of the
species, revardcless of its final resting place generically.

Types —Holotype and paratype, U. S. Geological Survey, to be
deposited in the U. S. National Museum.

Occurrence.—York District, Seward Peninsula, Alaska. The
holotype is labeled “On crest of ridge between Cassiterite Creek
and Lost River, about 5000’ N.12W. of Cassiterite Mine.” The
paratype, a specimen polished from a weathered lateral surface,
was found “in place, in bed of Rapid River, about 3500’ from
mouth of River.”

ACKNOWLEDGMENT

The cost of photography and illustration has been met by the
Faber Publication Fund of the University of Cincinnati Museum.
Many of the photographs are the work of Mr. Clifton Smith,
student assistant in the museum.

ADDENDUM

In order to avoid confusion, it is necessary to call attention to
the relationship of this work with a paper entitled “Notes on
Structure and Phylogeny of eurysiphonate Cephalopods,” appear-
ing in vol. 3, No. 13 of the Palzontographica Americana. The
present study was completed first and contains evidence of struc-
ture which is only summarized in the Paleontographica paper.
The views here presented tentatively concerning the significance
of the structures within the complex connecting rings have found
further support in the investigation of additional material, and
indeed, have been carried much further, tracing relationships not
only of the Ellesmeroceratide and the Tarphyceratide, but the
Endoceroidea and Actinoceroidea.

18 BULLETIN 102 36

REFERENCES

Flower, R. H.
Notes on struccure and phylogeny of ecurysiphonate cephalo-
pods, Paleontographica Americana, vol. 3, No. 1, Noy. 1941.

Foerste, A. F.
Notes on arctic Ordovician and Silurian cephalopods chiefly
from Boothia Felix-King William Land. Bache Peninsula, and
Bear Harbour, Denison Univ. Bull., Sei. Lab., Jour., vol. 19,
1921, pp. 247-306, pls. 27-35.

Kobayashi, T.
Faunal study of the Wanwanian () asal O dovician) series with
special notes on the Ribeiride and the Lllesmeroceroids, Imp.
Univ. Tokyo, Fac. Sci., Jour., Sec. II, vol. 3, 1933, pp. 249-328,
plssleO:
On the phylogeny of the primitive nautiloids, with descriptions
of Plectronoceras liaotungense, new species, and Iddingsia (?)
shantungensis, new species, Japanese Jour. Geol., Geogr., vol.
12, 1935, pp. 17-28, pl. 6.

Miller, A. K., and Thompson, M. L.
Beitriige zur Kenntniss tropisch-amerikanischer Tertiarmol-
lusken. VI. Some Tertiary nautiloids from Venezuela and Trin-
idad. Eeologe geologice Helvetiw, vol. 30, 1937, pp. 59-73,
pls. 7-10, text figs. 1-3.

Ruedemann, R.
Cephalopods of the Champlain Basin, New York State Museum
Bull. 90, 1906, 611 pp., 38 pls., 57 text figs.

Ulrich, E. O., and Foerste, A. F.
New genera of Ozarkian and Canadian cephalopods, Denison
Univ. Bull., Sci. Lab., Jour., vol. 30, 1935, pp. 259-290, pl. 38.

PLATES
PIC Aue m2)

Figure

BULLETIN 102

EXPLANATION OF PLATE 1 (2)

1-10. Ellesmeroceras bridgei Flower, n. sp. a 2 oe

Syntypes, float in Cassiterite Creek, York district, Seward
Peninsula, Alaska.

Ventral view of specimen, showing exfoliated siphunele.

il
2-4. Ventral, lateral and dorsal views of specimen retaining sutures.
5- 6. Cross sections of spee'men at intervals of 28 mm.

Ue

Venter of broken specimen, showing annulated in‘erior of. si-
oD
phunele. (Same sp. as PI. 2, fig. 6.)

8-9. Longitudinal section of specimen X1, and enlarged, showing si-
tan] 4 : z Fon) i h) é SD
phuneular structure and inorganic deposit simulating dis-
sepiments.

10. Venter of apical half of same specimen figure 1, ground to show
siphuncular outline.

38

Page

7

No. 102, Pu. 1

Buu. AMER. PALEONT.

Pu. 2, VOL. 27

¥

] sg 4 e mai 2 ot
iy s int sy ' ne » ‘

Y Pi AG

7
| ; ; We i \
j ' *

Wis ‘> wy iy i

READE 20 @)

22 3ULLETIN 102 40

EXPLANATION OF PLATE 2 (3)

Mera Ia oe
Figure Page
1-2. Plectoceras sewardense Flower, n. sp. 14

1. Holotype X1, lateral.
2. Paratype, longitudinal section. Cassiterite Creek,
Seward Peninsula, Alaska.
3-5. Ellesmeroceras expansum Flower, n. sp. : of eet)
Lateral, apical and adoral views of holotype. Float of
Cassiterite Creek, Seward Peninsula, Alaska.
6. Ellesmeroceras bridgei Flower, n. sp. __.._-..__---.__-- eee fi
Dorsal wall of siphuncle showing relation of necks and
thickened siphunele wall.

AMER. PALEONT

BULL.

Pi. 3, VOL. 27

oy
Ai

aA tn
eel: rete 8 aaa

(Nos; 55-58). 314 pp., 80 pls. 2. 6.00
Mainly Ecuadoran, Peruvian and Mexican Tertiary
forams and mollusks and Paleozoic fossils.

(Nos. 59-61), 140 pp., 48 pls. ; Pap av. eee DOO
Venezuela and Trinidad Tertiary “Mollusca.
CONG 62-63) -% 295. Dis oo DI Sse ce eS 6,00
Peruvian Tertiary Mollusea.
(Nos. 64-67), 286 pp., 29 pls. — . eecee rT eib-00
Mainly Tertiary Mollusca and Cretaceous “corals.
CNG.) Pe be DD ied PIS sere ae ba ae ee Se 5.00
Tertiary Paleontology, Peru.
XX. (Nos. 69-70C). 266 pp., 26 pls. — ._.. 6.09
Cretaceous and Tertiary Paleontology of Pern and Cuba.
BRASS -(Nos. 71-72)... 321 pp., i2 pls. = Sab eaa es aeeabo7s ate SA
Paleozoic Paleont aloey and Séeatigraphy.
EX:?. (Nos. 73-76). 356 pp., 31 pls. as, se SN OD
Paleozoic Paleontclogy and Tertiary Foraminifera.
mXiit (Nos. 77-79). 251 pp., 35 pls, -..- s 5.00
Corals, Cretaceous micro-suna and biography ae ‘Gonrad.
SKS. (Nos, 80-87); 3384 ppij227 plss paves eee THEY)
Mainly Paleozoic faunas and Tertiary Mollusca.
XXV. (Nos. 88-94B). 306 pp., 30 pls. Se ag; 7.09

Paleozoic fossils of Ontario, Oklahoma and Colombia,
Mesozoie echinoids, California Pleistocene and Maryland
Miocene mollusks.

XXVI. (Nos. 95-100). 420 pp., 58 pls. . eS : : =iipeicy Soseerarsoy fa 114)
Florida Recent marine sheils, Texas Cretaceous fossils,
Cuban Cretaceous corals, and geology and paleontology
of Ecuador.

PALA ONTOGRAPHICA AMERICANA

Vo'ume I. (Nos. 1-5). 519 pp., 75 pls. — ... $12.00
Monographs of arcas, Lutetia, rudisti ds and venerids.
Volume II No’s 6- i2 ese Nai $12.00
Volume ITI
Number ‘

18

© BULLETINS <=,
Y = _ APR 7 194g °
é OF tla RAaY

AMERICAN
PALEONTOLOGY

RN ES ae SC —————————————

“VOL. XXVII

lgo42

Paleontological Research Institution

Ithaca, New York
tS Pe

CONDENSED TABLE OF CONTENTS OF BULLETINS OF AMERICAN

PALEONTOLOGY AND PALZONTOGRAPHICA AMERICANA*

BULLETINS OF AMERICAN PALEONTOLOGY

Volume’'I.° (Nos: 125): 854 cpp... 82plsi 3 ae ea ee ep AeeOM
Mainly Tertiary Mollusca.
II. (Nos. 6-10). 347 pp., 28 pls. —._~ a Siete lee OG
Tertiary Mollusca and Foraminifera, ale ouole Raunae
Ill. (Nos. 11-15). 402 pp., 29 pls. —_ SONEOR ign ae hE ade Oooo 8.00
Mainly Tertiary Mollusca and Paleozoic sections and
faunas.
IV. (Nos, 16-21). 161 pp., 26 pls. Spee oc OU)

Mainly Tertiary Mollusca and sections ae ‘Palenzoien: sec-
tions and faunas.
V. (Nos. 22-30). 437 pp., 68 pls. -. 8.00
Tertiary fossils mainly Santo Dominean, ‘Mesozoic ‘gud
Paleozoic fossils.
VI-=€No.' 3) 2<- 268. ppi77 59. pls. ee taUiee ene Waker amar N een ae: Oe prs, LORIE,
Claibornian Eocene pelecypods.
VIEs | GNO2 32) ce (3804pp 2 90. pls 2 ans 12.00
Claibornian Eocene scaphopods, ‘gastropods. and cephalo:
pods.
VIII. (Nos. 33-36). 357 pp., 15 pls. : Beer oe ci en YL x 5.00
Mainly Tertiary Mollusca.
IX. (Nos. 37-39). ~462.-pp., 35 pls. ro AMM paubo me So 4
Tertiary Mollusca mainly from Costa ‘Rica.
X. (Nos. 40-42), 382 pp., 54 pls. 8.00
Tertiary forams and mollusks mainly. from “Trinidad ‘and
Paleozoic fossils.
XI. (Nos. 43-46). 272 pp., 41 pls. a PML tere FN 3 |)
Tertiary, Mesozoic ane Paleozoic fossils mainly from
Venezuela.
XII. (Nos. 47-48), 494 pp., 8 pls. i soe OCU
Venezuela and Trinidad forams and Mesozoic invertes
brate bibliography.
XIII. (Nos. 49-50). 264 pp., 47 pls. _ 6.00
Venezuelan Tertiary Mollusea and Tertiary Maniwalia.
XIV. (Nos. 51-54), 806 pp., 44 pls. 6.50
Mexican Tertiary forams and Tertiary mollusks of Peru
and Colombia.

* Complete titles and price list of all numbers may be had. on applica-
sion. All volumes available.

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 103

AN ARCTIC CEPHALOPOD FAUNULE FROM THE
CYNTHIANA OF KENTUCKY

By

Rousseau H. Flower

March 30, 1942

PALEONTOLOGICAL RESEARCH INSTITUTION

TItHAcA, NEw YORK

Ils Sb Z\.

oo i an le

vr
=

0 SP Fe
YAHOO. CV OS CA?

Coit WUE

CONTENTS

Page

Tawa di CitOn enero wn were ee RAE Tr se se 5
TE LRESSU AYE UCNO a ea cS S oO ee a Se 6
Baunale Hela sioushipsmeews: reset eel le 8
Rysuem nice CSCraiy NOMS Retest ee 12
lass 2 Cephalopod aapuemeer eekeeres SA ele ee ee 12
Ordo rveN a UiiOld lmine ee oe < 20s itera duel Lent dee Soeeetaaat t 12
SulbordersEmysiphonsdtalncs i. ta. See ee Pie 2
Supertamily Actinoceroidea 4.1... ee 12

HamMUlyee SACtOCenAtlG Dy y= sk ae ee AL ee 12

Genus Mreptoceras Plower, n.-gen, 2 15

T. persiphonatum PWlower,n.sp. 17

i perseptatum Blower, newwp. .. 0) 18

i prenuntimn Mower, nl. isp... ee 19
SupordersStenosiphomatay ee. eee ee ee 20
Ranailyaphizoceratiden =A te ee ees Po ee ee 20

Cena WurvizOcenaineetat nn 24 24.0 .0oe etre tl ell tas 20

Re graciitorme: Mower, n: Sp. 0... 21

Re RCOMMCUIMIUE LOWED ye tly Spo tensa) cen en ee: 21

iRancnulys Oncocenatidess 2 iu Sty) WO) te 22

Genus: Neumatocenis! 258 fo ie 22

Neecanlsomi Hower Weiss .2. .5 5) ee 23

Bamully Oonoceratider: eg ee 24

Conus OO Ocetan mens. tee. ett ea. Poy) eo) ee eed ee 24

©} planiseptatumy Blower, n-/sp. 8 ae 31

Ox;acutum Mlower me /sp. 2h... 2... ee 32

OF? sorevidomunm: Plower, n- sp... 33

©. multicameratim Flower, n. sp. _.....c.----cecccee---e--s- 34

©. gracilicurvatum Wlower, m: sp. 22... 39

Om inangulatum: Mower, n. sp. 2 36

O. triangulatum var. cylindratum Flower, n. sp. 3

O. suborthoforme Flower, n. Sse eee eee oe see ee 38

Dino ee S COC EGA ser ss aia eel ee St a 38

WD TESTO COTA SI geet caste SNE DE CO Re secy Beta es 38

UB) esto S 1) iene pect ener Ae COL Le ore Yeh g dere eae 38

RUC CN GMCS Gamer ee EEN Nace wt Po St ee Ae ep ee neat 40

TPAIG NIELS) <a tan Ua OS eee See Se en POEL, SOUS UNE, hy 10 Yel 43

AN ARCTIC CEPHALOPOD FAUNULE
FROM THE CYNTHIANA OF KENTUCKY
By
Rousseau H. FLOWER

University of Cincinnati

INTRODUCTION

The cephalopods described in the following pages are known
only from a lens exposed on the southeast side of the Poindexter
quarry (Dunn, 1930), at the outskirts of Cynthiana, Kentucky,
on the west side of the main road leading to Paris and Lexington.
The faunule occurs high in the wall of the quarry among dense
and relatively barren limestones and underlies fossiliferous beds
carrying abundant Orthorhynchula. The entire series of beds lies
within the Nicholas limestone (Foerste, 1909, pp. 209, 210),
which is properly referred to the Greendale member of the Cyn-
thiana limestone (McFarlan, 1938, pp. 992-995, also fide litt).

The cephalopod association is remarkable in many of its
features. Faunally, it is quite distinct, consisting of new species
which have not been found elsewhere in the Cynthiana. More
remarkable is the fact that few of the species have close relatives
in the remainder of the Cynthiana or in any of the Ordovician
strata of the Cincinnati arch. Instead, there are represented here,
genera which have been previously known largely, if not entirely,
from the arctic region of North America, and which have come
to be considered diagnostic of the post-Trenton, and even Rich-
mond, age of the strata in which they occur. The present study
adds to the list of supposedly late Ordovician genera which are
now definitely established as occurring in the Trenton. The as-
sociation is unusual, also, in the vertical position of most of the
cephalopods, a condition which is attributed to burial of the conch
while some gas was still retained in the phragmocone, as dis-
cussed below.

The material which forms the basis of this study was collected
by the writer and is deposited in the Museum of the University of
Cincinnati. The Faber Publication Fund of the University
Museum has defrayed the cost of illustrations.

6 BULLETIN 103 46

PRESERVATION

The mode of preservation of the cephalopods shows several
features of unusual interest which make possible a reconstruction
of the conditions under which the shells were buried. The lens.
now exposed in the wall of the quarry, is only a section across a
channel filling, about one and a half feet thick and four feet in
width. Conversation with the quarrymen revealed that the ceph-
alopods had been encountered extending far out into the quarry
in rock now long since removed, but the band in which they oc-
curred remained narrow. This supports the belief, founded upon
the appearance of the lens in its present condition, that it repre-
sents a section across a linear channel filling.

The lower part of the lens contains pelecypods and gastropods
in some abundance, but its upper three-fourths is occupied al-
most exclusively by cephalopods. Cyrtoceracones of the genus
Oonoceras are the dominant element, and nearly all of the shells
occur in a vertical position with the apex directed upward. This
evidently has nothing to do with the fact that cyrtoceracones
normally held the shell in this position during life, as has been
demonstrated by color bands reported for a great variety of gen-
era ranging from Ordovician to Mississippian. Cephalopods
could hardly be preserved in a natural vertical position unless
they were burrowers; pelecypods are not infrequently found in
their life position, particularly in the Upper Devonian of New
York and Pennsylvania, but these are forms which have lived be-
neath the surface of the sea bottom. The cephalopods of the
Cynthiana lens are orthoceracones, cyrtoceracones and _ brevi-
cones ; forms which were not only motile, but were probably not
greatly dependent upon a substratum. The prevalent invasion of
matrix into the living chambers shows conclusively that the as-
sociation 1s a thanatoccenose, and that the shells not only were
dead, but free of the body mass of their former occupants when
buried.

The vertical position of the shells can be explained only by the
presence of gas in the camere at the time of burial. Gas in suffi-
cient quantity will cause a cephalopod shell to float, but if only a
small quantity is present the shell will come to rest on the bottom
with the camerated portion of the shell directed upward as is seen
here. This is quite possible from the condition of the shells. Ap-

47 CYNTHIANA CEPHALOPODS: FLOWER il

parently they were buried while the phragmocone was intact, or
very largely so, for it is always free from sediment, though filled
by crystalline calcite which was evidently deposited there sub-
sequent to burial and the removal of the gas by solution. Quite
possibly the shells were transported some distance before sinking
to the bottom and being washed to their present location; cer-
tainly the complete absence of conspecific forms outside of the
lens suggests that the shells did not live in the immediate vicinity.
On the other hand, it seems improbable that such shells could
have been carried any considerable distance without showing
more breakage of the aperture and some loss of surface features
as a result of solution or abrasion.

Subsequent to the burial of the shells, a considerable interval
of time must have elapsed, after which the strata in which they
were deposited were worn down, probably by current and wave
action. In this interval, calcite was deposited inorganically in
thé camere of the shells. When the upper part of the bed was re-
moved, the uppermost parts of the cephalopod shells were re-
moved also, but sediment failed to penetrate the camere, showing
that the calcite deposition occurred prior to the deposition of sedi-
ments on the abraded surface of this lens. This feature is prob-
ably of no major significance as a diastemic break, but was
probably only an extremely local phenomenon. It is important,
however, in showing that, very soon after burial, calcite may be
deposited inorganically in a marine shell in cavities not occupied
by sediment. An even more startling example of this phenom-
enon has been found by the writer in reef associations of the
Valcour limestone, upper Chazy, of the Champlain Valley, New
York, where the condition of the shells shows conclusively that
they were buried, filled with calcite, then excavated by waves,
washed about and broken, and finally buried in a black lime mud,
Here typical specimens terminate in irregular surfaces of calcite,
which clearly represent broken surfaces and have no connection
with any organic structures.

8 BULLETIN 103 48

FAUNAE RE EATIONSEMBRS

The species of cephalopods which have been found in the
Cynthiana limestone in the faunule described above have not been
found elsewhere in the Ordovician of Kentucky. Their signifi-
cance, however, lies not so much in the fact that they are appar-
ently confined to this single locality and horizon, but in their
strong affinities with cephalopods from quite distant regions, in
various aspects of the arctic Ordovician fauna. This is to be found
in the Cape Calhoun beds of Greenland, various localities in the
Arctic Archipellago, the Nelson River and Shamattawa lime-
stones of Hudson Bay, the Liskeard limestone of Lake Timisk-
aming, the Whitehead formation of Gaspé, and some of the
Ordovician strata of Anticosti, particularly the Vaureal lime-
stone, the Red River series of Manitoba, the Bighorn formation
of Wyoming, and the Fremont limestone of Colorado. There is
still much uncertainty concerning the age of these formations.
They have been considered Trenton, Richmond, and Covington
equivalents, and the suggestion has been put forward that they
may represent deposits ranging from the Trenton through the
Richmond. A number of cephalopod genera which are character-
istic of these beds have come to be considered diagnostic of the
Richmond, or, at least, of the post-Trenton age of the strata, for
many are absent in the typical Richmond. Several of these genera
have subsequently been found in the Stewartville dolomite of Min-
nesota (Kay, 1935, p. 587), including Lambeoceras, W estonoc-
eras, Diestoceras, Charactoceras and Ephippiorthoceras. The
Cynthiana faunule adds to the list of supposedly diagnostic Rich-
mond genera which are now known to occur in the Trenton,
Neumatoceras and Oonoceras, while representatives of more
widespread genera show closest affinities with species of the arctic
association.

This is significant, also, in that it demonstrates a connection
between the east-central embayment in late Trenton time and the
arctic embayment, a connection which does not seem to have been

49 CYNTHIANA CEPHALOPODS: FLOWER 9

previously suspected. Foerste (1932, p. 54) quotes Ulrich, ap-
parently concurring in his view, that the Cathys' of Tennessee
and Kentucky, the Fairview, and the Arnheim carry faunas which
invaded the continent from the south, while the underlying
strata, the Bigby and Lexington, the Eden and lower Maysville,
and the Belleview-Mt. Auburn sequence of the upper Maysville,
carry a fauna of north Atlantic origin. The cephalopods described
here show evidence of a close relationship between the arctic em-
bayment and the Cynthiana. This suggests strongly that the evi-
dence leading to the conclusion stated above might be reéxamined
with profit.

Of the cephalopod genera found in the Cynthiana faunule, only
Treptoceras appears to be indigenous to the Cincinnati-Jessamine
region. The genus is the one most commonly encountered from
the Cynthiana to the top of the Richmond; it is developed in the
Richmond of southern Ontario and in the Lorraine of western
New York. Three species are described from the faunule con-
sidered here. Of these, two species, 7. perseptatum and T. pre-
nuntium, appear to be closely related to forms from the Cincin-
natian strata. The third, 7. perseptatum, is a form with exceed-
ingly shallow camere and a markedly eccentric siphuncle. The
eccentric siphuncle distinguishes it from 7. mulleri ( Foerste, 1910,
pl. 1, fig. 5), but it appears to differ less from some Richmond
forms not known to occur below the Waynesville in the Cincin-
nati area.

Oonoceras is the dominant genus of the Cynthiana lens faunule,
being represented by six species and one variety. The genus, as
revised below, contains species which have formerly been placed
in Beloitoceras and Richardsonoceras. As pointed out under the
discussion of the genus, it may represent a form group rather
than a genetic unit and does not appear to be set off sharply from
Cyrtorizoceras or Beloitoceras. The only species of the genus
known elsewhere from the Cynthiana is one which is relatively

1 The Cathys is typically developed in Tennessee, but that name is no
longer applied to the Kentucky region. The Cathys is the equivalent of
the Cynthiana, both being uppermost Trenton in their respective areas.
Until relatively recently the name Bigby, which typically underlies the
Cathys in Tennessee, was applied to the Lexington of Kentucky.

10 BULLETIN 103 50

rapidly expanding, and, as a result, actually not typical of the
genus in form. As this form is known only from the phragmo-
cone, it might be placed as easily in Beloitoceras or Cyrtorizoceras.

Cyrtoceracones typical of Oonoceras in form are known only
from faunas of arctic affinities in America. Oonoceras obstructum
(Foerste, 1928, p. 307, pl. 52, figs. 2-3) was described from the
Vaureal formation of Anticosti Island as a species of Beloitoceras.
This species agrees with O. multicameratum, described below, in
the dorsal constriction of the interior of the mature living cham-
ber, a feature not noted in other species of the genus. The Anti-
costi species is much larger than that of the Cynthiana and has
considerably deeper camerz. Nevertheless the two forms are so
strikingly similar as to suggest a much closer relationship than
is expressed by the inclusion of both in a single rather large genus.

The Ordovician strata of Hudson Bay supply other species
referable to Oonoceras. Oonoceras shamattawense (Foerste and
Savage, 1927, p. 78, pl. 15, figs. 2a-b), originally placed in the
actinosiphonate genus Oocerina, is typical of Oonoceras in form
and siphuncle, but differs from other species in that the sutures
rise farther orad on the dorsum than on the venter. Two Silurian
species were referred to the genus Oocerina in the same paper,
both from the Attawapiskat limestone. One of these ( Foerste and
Savage, 1927, p. 8o, pl. 14, fig. 4) appears, from the illustration
and description, to be a typical member of the genus. If so, it is
the only Silurian representative of the genus known in America.
The other (Foerste and Savage, 1927, p. 79, pl. 14, fie. 2A=@)
has a very broad siphuncle suggesting an actinoceroid cephalopod
and is apparently not related to Oonoceras.

The Bighorn formation has yielded two representatives of the
genus, both originally referred to Richardsonoceras. The reason
for the change of generic references is given under the discussion
of Oonoceras below. They are strikingly similar to two of the
species of the Cynthiana. Oonoceras wyonungense (Foerste,
1935, p. 40, pl. 3, fig. 1) is quite similar to Oonoceras plantsep-
tatum in section and general aspect, though it is a much larger
species, and the camere are slightly deeper in proportion to the
size of the conch. Oonoceras subcuneatum (Foerste, 1935, p. 41,
pl. 7, figs. 3-4) is comparable in section and in its very shallow

51 CYNTHIANA CEPHALOPODS: FLOWER ilal

camere to O. acutum of the Cynthiana, but the section is even
more compressed and subangular on the venter.

Neumatoceras carlsoni furnishes the first record for the genus
in southeastern North America and also the first occurrence of
the genus in beds of undisputable Middle Ordovician age. The
genus is typically developed in the Bighorn formation of Wyom-
ing and the Fremont limestone of Colorado (Foerste, 1935, pp.
31-32), and is also well represented in the Whitehead formation
of Gaspé (Foerste, 1936, p. 380). It is doubtfully represented in
the Shamattawa limestone of Hudson Bay by lVestonoceras (?)
contractum Foerste and Savage (1927, p. 55, pl 16, figs. 2A-B).
Foerste has pointed out the possible connection of this form with
Neumatoceras and with several other inadequately known species,
including Wuinnipegoceras, sp. from the Red River formation of
Manitoba and Oncoceras tumidwm Schuchert from the Ordo-
vician of Baffin Land (Foerste, 1935, p. 32). In addition, the
genus is doubtfully represented in the Gonioceras Bay formation
by Maelonoceras reclinatum Troedsson (1926, p. 91, pl. 55, figs.
1-3). This is a species which exhibits the strong lateral contrac-
tion of the mature part of the shell which is typical of the genus
and shows a siphuncle very similar to that of N. carlsoni. It fails,
however, to attain the extreme vertical gibbosity which is such a
conspicuous feature of typical members of the genus. The exact
correlation of the Gonioceras Bay formation has not been deter-
mined, but much of the evidence suggests early Trenton age.

Diestoceras, while represented only by a specifically undeter-
minable fragment, suggests again the northern faunas, being well
developed in the Fremont limestone, the Bighorn formation, the
Red River, Shamattawa limestone, Cape Calhoun beds, the
Whitehead formation of Gaspé, and the Ordovician of Anticosti.
The genus is an exceedingly wide ranging one, however. It has
been reported from beds of Middle Ordovician age (Foerste, 1933,
pp. 145-146) and also from the Lower Ordovician of the Mingan
Islands (Eoerste, 1938, pp: 103-104, pl. 20, fig, @; pl. 21, figs:
yyiss)3
2 The two Chazyan species are not quite typical of the genus in form

and may eventually prove to be unrelated to Diestocerus. Nothing is known
of their internal structure.

12 BULLETIN 103 52

The presence of two species of Rizoceras again indicates
strongly a connection with the arctic fauna. Previously only two
species of Rizoceras have been reported from the American Ordo-
vician. One is Rizoceras carletonense Foerste (1932, pl. 34. fig.
4; 1933, p. 118) of the Black River limestone of the Ottawa
Valley. This does not show any close relationship to either of
our species. The other is R. coronatuwm Foerste and Savage
(1927, p. 50, pl. 5, fig. 7) of the Shamattawa limestone of Hudson
Bay. This species is quite similar to R. graciliforme in propor-
tions. While the relationship of the Ordovician species of Rig-
oceras to one another seems fairly certain, their connection with
the Silurian genotype remains to be established. A new genus,
still undescribed, has been found by the writer in the Chazyan of
the Champlain Valley, which differs from Rizoceras in the ortho-
choanitic siphuncle and the absence of a hyponomic sinus. The
Cynthiana forms and the other Ordovician forms may prove to be
closer to this genus than to typical Rizoceras when their internal
structure has been made known, but the presence of a well-defined
hyponomic sinus indicates that they are different enough to be
set apart from the Chazyan genus.

SYSUEMATIC. DESCRIPTIONS

Class CEPHALOPODA
Order NAUTILOIDEA
Suborder EURYSIPHONATA3
Superfamily ACTINOCEROIDEA
Family SACTOCERATIDZE

Because of confusion as to exactly what constitutes the genus
Loxoceras McCoy (a problem which has not yet been solved),
Troedsson (1926, p. 79) proposed the family Sactoceratide for
orthoceracones with small cyrtochoanitic siphuncles. He referred

3 The Eurysiphonata, originally proposed by Teichert and subsequently
used by him, was given the rank of a subelass. It is treated here as a sub-
order of the Nautiloidea, largely because it is felt that the subclasses
Tetrabranchiata and Dibranehiata and the orders Ammonoidea and Nauti-
loidea of the Tetrabranchiata are too widely known to be discarded. There
appears at the present time to be as good justification for the recognition
of the Eurysiphonata and Stenosiphonata as major divisions, but the rank
given to such divisions is unfortunately a matter of opinion upon which
it is difficult to come to any very wide agreement.

53 CYNTHIANA CEPHALOPODS: FLOWER 13

to it Sactoceras Hyatt and Eskimoceras Troedsson. However,
the genotype of Sactoceras is clearly an actinoceroid, and there-
fore Foerste and Teichert (1930, p. 208) correctly placed the
family in the Actinoceroidea, a new superfamily with essentially
the scope of the Actinoceratide of Hyatt. They redefined the
family and placed in it the genera Sactoceras, Eskimoceras,
Troedssonoceras, Ormoceras and Deiroceras. Miller, Dunbar,
and Condra (1933, p. 77) referred Pseudorthoceras, Mooreoceras
and Euloxoceras to the family. These genera were later made the
nucleus of a new family, Pseudorthoceratide Flower and Caster
(1935, pp. 29-30), which was subsequently shown to be unrelated
to the Actinoceroidea, but, derived, instead, from orthochoanitic
orthoceracones of the “Orthoceratide’’ (Flower, 1939, pp. 165-
180). Restudy of the genus Troedssonoceras (Flower, 1939, pp.
481-484) showed that it is a typical member of the Sactoceratide
closely allied to Deiroceras, although the Greenland species which
have been referred to it are not congeneric and cannot even be
placed in the Actinoceroidea (Teichert, 1934, pp. 40-42) and must
therefore be assigned to a different genus, for which a new name
had already been provided by Shimizu and Obata (1935) along
with a great many others, most of which seem to have no good
use. The writer subsequently discussed the Sactoceratidz briefly
(1940, pp. 442-443), pointing out the probable relationship of
Rayonnoceras and urging that the form of the radial canals might
serve as a better criterion of the group than the form of the si-
phuncular segments.

Several grave problems remain, particularly in the matter of
determining generic boundaries. The writer (1939, p. 24; 1940,
p. 443) has several times mentioned the difficulites involved in
the placing of some Ordovician species which obviously belong to
a single generic group and which are prevalent in the Cincin- ,
natian. The main difficulty lies in the various ontogenetic stages
encountered in a single individual, each of which is characteristic
of a described genus. The early segments are very similar to those
of Armenoceras. These become more slender, the necks less
strongly recurved, and they thus attain the condition typical of
Ormoceras. Subsequently, the siphuncle becomes more slender,
approximating the condition of typical Dezroceras, and further

14 BULLETIN 103 54

simplification of the outline results in the outline typical of
Leurorthoceras. Such changes in the ontogeny are nothing new.
A problem arises from the fact that species which have been re-
ferred to these genera in the past are represented by fragments of
the conchs Leuwrorthcceras is known only from adoral portions
of large individuals. It cannot be determined what type of si-
phuncular outline occurs in earlier stages, because such earlier
stages are unknown for the genotype. The same applies to
Deiroceras. It is likewise not definitely known whether the early
stages of Ormoceras are Armenoceras-like in siphuncular out-
line. Silurian and Devonian species, in which the genotype of
Ormoceras is included, are known to retain siphuncular segments
typical of Ormoccrcs throughout life, without the appearance of
Deiroceras or Leurorthoceras stages. In this respect, it offers a
sharp contrast to the Ordovician species, which retain a high de-
gree of plasticity of siphuncular outline during life. It seems highly
desirable that the group of plastic species should be placed in a
separate genus rather than in Ormoceras.

Paractinoceras Hyatt (1900, p. 528, see also Foerste, 1920, pp.
209-210) of the Ordovician shows an adoral simplification of
siphuncular outline, but it cannct be used for the species under
consideration because the early siphuncular stages are those of
Actinoceras rather than of Armenoceras. The conch shows an
adoral cont-action which is essentially a feature of the Actinocer-
atidze, not known in any of the Sactoceratide.

The differentiation between Sactoceras and Ormoceras seems
to be a matter which has not been adequately treated. Ormoceras
has frequently been compared with other actinoceroids, in partic-
ular with Armenoceras and Actinoceras, but descriptions of
Sactoceras rarely mention any genus other than Losxoceras by
way of comparison. In the opinion of the writer, there is really
no geod distinction between Sactoceras and Ormoceras. The
genotype of Sactoceras shows the necks to be somewhat shorter
and the brims somewhat better developed than in Ormocevas, but
there is variability in both genera in this respect which supplies
complete intergradation. The segments of the siphuncle in the
two genera are almost identical in form, and neither shows any

55 CYNTHIANA CEPHALOPODS: FLOWER 15

close resemblance to the Armenoceras-like segments of the Ordo-
vician species. The position of the siphuncle in both genera may
vary from subcentral to a position close to the ventral wall. The
sutures may be straight and transverse or slightly inclined apicad
on the venter. Only lack of access to specimens of the genotype
of Sactoceras causes the writer to refrain from formally reducing
Sactoceras to synonymy and proposing a new family name based
upon Ormoceras.

The separation of the plastic Ordovician species into a new
genus distinct from Sactoceras and Ormoceras is clearly desir-
able. However, there is no certainty that this new genus, named
Treptoceras below, may not eventually prove to be a synonym of
Leurorthoceras or of Deiroceras. It is even possible, though not
probable in the opinion of the writer, that these two genera may
not be distinct when their genotypes are known from reasonably
complete specimens. However, it seems that there is a real ad-
vantage at the present time for the proposal of a genus for these
numerous Ordovician species, which can be fully defined and
recognized easily. If subsequent study should show that it is a
synonym of Deiroceras or Leurorthoceras, or both, the transfer
will be a relatively simple one.

Only one more obstacle to the proposal of this genus need be
considered. This is the fact that Shimizu and Obata (1935A, pp.
27-35) have already proposed not only a genus, but a whole fam-
ily including several genera, which might possibly embrace these
forms. The genera are based upon intricacies of siphuncular out-
line of supposedly mature individuals depending upon features
which, in the opinion of the writer, are probably not greater than
specific in rank. Further, they take no account of the variation
of the siphuncular outline in ontogeny and cannot be demonstrated
to be congeneric with Treptoceras until they are at least ade-
quately described and much more fully illustrated.

Genus TREPTOCERAS Flower, n. gen.
Genotype.—Orthoceras dusert Miller
Conch orthoceraconic, circular or slightly depressed in section,

with sutures straight and either transverse or sloping slightly api-
cad from dorsum to venter. The septa are normally very shal-

16 BULLETIN 103 56

lowly curved, the camere are usually shallow, though this is not
uniform. The siphuncle is located some distance ventrad of the
certer in mature positions of the shell, but may be central or sub-
central in the young stages The siphuncular outline is highly
plastic. The earliest segments are /rmenoceras-like in outline,
broader than long and frequently heart-shaped, being broadest
ot the adoral end, sloping gradually and converging adapically
with a relatively small area of adnation between the adapical end
of the connecting ring and the septum. The necks at this stage are
strongly recurved and recumbent or nearly so; the connecting
ring adjacent to the brim 1s frequently in contact with the septum.
Segments farther orad become more slender, with the brim free,
the segment subglobular, as is typical of Ormoceras, though the
necks are usually shorter and more sharply recurved at this stage
than is typical of Ormoceras. Farther orad the segments take on
the slencer outline of Deiroceras and finally of Leuwrorthoceras,
though that condition is not attained in the gerontic stage of all
species. |

Deposits within the siphuncle are typical of the Sactoceratide,
and the radial canals are straight and perpendicular to the central
canal. Apparently the radial canals are few in number, for many
sections fail to show them at all, but show instead the appearance
of a continuous lining as in the Pseudorthoceratide. The peri-
spatium is always developed, however, and serves to distinguish
Treptoceras under such circumstances.

Discussion.—The salient features and the problems of nomen-
clature have been discussed above. The genus is one which is
very widespread in the Upper Ordovician of the Cincinnati region,
and one also represented in the Middle Ordovician. Quite prob-
ably it contains a number of species formerly placed in Ormoceras
and Deiroceras. These include Deiroceras dismukense Foerste
and Teichert (1935) of the Richmond of Tennessee, Ormoceras
(?) covingtonense Foerste and Teichert of the Maysville of Ken-
tucky, Deiroceras curdsvillense Foerste and Teichert of the
Curdsville member of the Trenton of Tennessee, Ormoceras caz-
nonense Foerste and Teichert of the Cannon member of the
Trenton of Nashville, Tennessee, Ormoceras troosti Foerste and
Teichert of the Cathys of Tennessee, Ormoceras lin:’sleyi Foreste

CYNTHIANA CEPHALOPODS: FLOWER 7

or
~

and Teichert of the Trenton of Tennessee. To these should be
added practically all of the smooth-shelled species of “Orthoceras”
described from the Cincinnati region from the Cynthiana to the
top of the Richmond. Also are included many of the straight-
shelled’ cephalopods of the Lorraine group of New York, which
were largely referred to Paractinoceras and Actinoceras by
Ruedemann (1926) and are closely related to species of the same
age in the Cincinnati region. The species selected as a type,
Orthoceras duseri Miller, is one of the more abundant and better
known forms of the Waynesville formation of the Richmond of

the Cincinnati area.

Treptoceras persiphonatum Flower, n. sp. Plate 4, figs. 1-2

This species is represented only by the holotype. The section
is circular, expanding from 25 mm. to 32 mm. in the 75 mm. of
the phragmocone, and to 39 mm. in the 60 mm. extent of the liv-
ing chamber. The sutures are straight and transverse. The cam-
ere occur uniformly four and a half in a length equal to the adoral
diameter of the shell. The septum is shallow, the depth of curva-
ture being 3.6 mm. at a conchial diameter of 30 mm., or approxi-
mately one-ninth the diameter. The siphuncle is markedly
eccentric. At the apical end of the type, it is 4 mm. in diameter
within the camera and 3 mm. from the ventral wall of the shell.
At the adoral end, it is of uncertain diameter, but its center lies
7 mm. from the venter. The segments are slightly longer than
broad, as is to be expected from the growth stage represented.
A segment, 7 mm. long, expands from 4 mm, to 6 mm, within the
camere. The septal neck is one-seventh the length of the seg-
ment, the brim is slightly less than the neck, and the area of ad-
nation is vestigial. Deposits are present in the siphuncle through-
out ; those at the adoral end are not fully developed. Deposits are .
not developed in the camere so far as can be determined from the
recrystallized condition of the specimen. The internal mold is
smooth. None of the shell surface is preserved.

T ype—Holotype, Univ. of Cincinnati, No. 22695.

Occurrence-—From the Greendale member of the Cynthiana

limestone, Cynthiana, Kentucky.

18 BULLETIN 103 58

Treptoceras perseptatum Flower, n. sp. Plate 1, fig. 1; Plate 3, fig. 6

Section circular throughout, with straight transverse sutures.
The conch expands from 16 mm, to 21 mm. in a length of 40 mm.,
the rate being 5 mm. in a length of zo mm. throughout the phrag-
mocone. The sutures are straight and transverse. Camere occur
twelve in a length equal to the adoral diameter of the shell, but
the last two or three may be even shallower in a mature shell.
The septa have a depth of 3.6 mm. at a conchial diameter of 30
mm., approximately one-ninth the diameter and equal to the
depth of one and a half camere. The siphuncle is central at a
diameter of 14 mm.,, but becomes eccentric rapidly, lying with
its center 7 mm. from the venter and 9 mm. from the dorsum at
a diameter of 16 mm., and only 2 mm. from the venter at a
conchial diameter of 21 mm. The siphuncular segments are
broader than high, a condition which often accompanies very shal-
low camer. At a conchial diameter of 15 mm., a segment is I.5
mm. long and expands from 2 mm. to 4 mm, within the camere.
Adorally the segments become more slender, so that, where the
length is 2 mm., the siphuncle expands from 2 mm. to 3 mm.
Deposits within the siphuncle are typical of the genus. Cameral
deposits are largely mural, but circuli appear outside the septal
necks.

A paratype supplies information concerning the mature living
chamber which has a basal diameter of 22 mm. and is 56 mm. in
length. Expansion is normal nearly to the middle of the living
chamber, where the vertical outline becomes convex, at least on
the preserved dorso-lateral surface. The apertural diameter is
estimated as 24 mm.

Discussion.—The apical siphuncular segments of this species
are very suggestive of Armenoceras, with the brim considerably
better developed than the neck. Adorally, the condition becomes
more similar to that of Ormoceras. The species shows a strong
similarity to Treptoceras milleri (Foerste, 1910, p. 76, pl. 1, fig.
5), a slightly larger form, but one with similar shallow camere.
T. persebtatum differs strikingly from this form in the rapid
movement, in ontogeny, of the siphuncle from the center to a
position close to the ventral wall. At a later stage, than that ever

59 CYNTHIANA CEPHALOPODS: FLOWER 19

attained in 7. perseptatum, judging by conchial diameters, 7. muil-
lert shows a much less eccentric siphuncle than does our species.

Both species, in their very shallow camere developed at a
relatively early stage of growth, offer a contrast to other species
known from the Trenton and Cincinnatian strata of the Cincin-
nati arch The next cccurrence of comparable forms is in the
Waynesville shales of the Richmond.

Types.—Univ. of Cincinnati, holotype, No. 22697, paratype,
No. 22608.

Occurrence—From the Greendale member of the Cynthiana
limestone, from Cynthiana, Kentucky.

Treptoceras prenuntium Flower, n. sp. Plate 1, fig. 2

Conch circular in section, expanding from 19 mm. to 25 mm.
in a length of 40 mm. The sutures are straight and transverse ;
seven camere occur in a length equal to an adoral diameter of
20 mm., and this proportion is constant throughout the known
portion of the shell. The septa are 4 mm. deep at a conchial
diameter of 19 mm., with the depth of curvature slightly greater
than the depth of the camera. As in T. perseptatum, the siphuncle
moves rapidly from a central position to a ventral one, but is not
as eccentric as in that species, moving from a subcentral position
at a conchial diameter of 11 mm., to one halfway between the cen-
ter and the venter at a conchial diameter of 25 mm. The siphun-
cular segments are usually faintly expanded, a segment 2.8 mm.
in length increasing in diameter from 1.5 mm, to 2.1 mm. The
maximum size of the species is not definitely known, as neither
gerontic camere nor living chambers have been observed, but the
condition of the siphuncular segments suggests that the phragmo-
cone did not continue very much further orad than is shown on.
the type.

Discussion.—The very slender siphuncular segments serve to
distinguish this species from its associates. It may also be readily
distinguished by the proportions of the conch; 7. perseptatum
has much shallower camere and a more eccentric siphuncle. T.
perisiphonatum shows a similar position of the siphuncle. Not only
are the segments broader in proportion to the conch, but the

20 BULLETIN 103 60

camere are also much deeper.
Types.—Univ. of Cincinnati, holotype, No. 22696; paratype,
No. 22697.
Occurrence.

From the Greendale member of the Cynthiana
limestone, at Cynthiana, Kentuck~.

Suborder STENOSIPHONATA
Family RIZOCERATID Hyatt
Genus RIZOCERAS Hyatt

Conch compressed, expanding with moderate rapidity, the apex
usually slightly curved exogastrically. The sutures are straight
and transverse. The siphuncle is placed close to the venter, which
is the more convex side of the conch; its segments slender but
clearly expanded within the camer, and free of any organic
deposit.

The conch is particularly characterized by the continuation of
the rather rapid rate of expansion to the aperture of the mature
shell. A hyponomic sinus is present throughout life, but the aper-
ture is otherwise unmodified. The surface markings are trans-
verse and retain the markings of the hyponomic sinus.

The relationship of the two species here described from the
Trenton of Kentucky has been adequately treated in the section
dealing with the faunal affinities of the Cynthiana lens and need
not be repeated. Rizoceras is apparently a long-ranging genus,
the oldest species being from the Black River of the Ottawa Val-
ley and persisting to the close of the Middle Silurian. It is better
represented in the Silurian of Bohemia than anywhere else; cer-
tainly the two species previously known from the American Ordo-
vician and the few American Silurian species, some of which are
inadequately known and rather atypical in form, do not make as
imposing an array as one might expect for a genus of such gen-
eralized aspect. The taxonomic relationship of Rigoceras is still
uncertain; quite probably it is, as Hyatt believed, a relatively
straight expression of the curved Cyrtorizoceras, but enough is
not known of the internal structure of the Ordovician species to
make this certain.

61 CYNTHIANA CEPHALOPODS: FLOWER 21

Rizoceras graciliforme Flower, n. sp. Plater 2 ation

This is a relatively small and slender Rizgoceras showing only
vestigial curvature in a faint concavity of the dorsum. The section
is circular at the base of the holotype where the diameter is 8 mm.
This increases in a length of 7 mm. to a height of 12 mm. and a
width of 11 mm. at the base of the living chamber. In 12 mm.,
the conch increases to 15 mm. and 17 mm. The aperture is not
clearly preserved except ventrolaterally, where faint indication of
the sinus is found.

The sutures bear very slight lateral lobes and are faintly in-
clined orad from dorsum to venter. The camere increase in the
length of the phragmocone from I mm. to 1.8 mm. No trace of
the siphuncle is preserved. The surface bears numerous fine and
closely spaced transverse markings. At regular intervals these
are thickened and elevated into vestigial annuli which are spaced
seven to eight in a length of 5 mm.

Discussion.—The slender form distinguishes this from the fol-
lowing species and gives it proportions somewhat similar to those
of R. coronatum Foerste and Savage of the Shamattawa lime-
stone of Hudson Bay. It may be distinguished readily from that
species by the smaller size, the development of slight lateral lobes,
and the faint obliquity of the sutures, those of that form being
straight and transverse.

Type.—Holotype, Univ. of Cincinnati, No. 22693.

Occurrence.—From the Greendale member of the Cynthiana
limestone, from Cynthiana, Kentucky.

Rizoceras conicum Flower, n. sp. Plate 1, figs. 7-8

Conch compressed, venter and dorsum equally rounded. Ven-
ter uniformly convex in vertical outline, dorsum concave adapi-
cally, nearly straight adorally; sides diverging uniformly. Height.
and width equal adapically, the section later becoming com-
pressed. The earliest stage observed has the height and width
both 6 mm. The holotype expands from 11 mm. and 11.5 mm. to
25 mm. and 23 mm. in a length of 20 mm. The phragmocone
terminates at a height of 13 mm. and a width of r2 mm. The
sutures are straight and transverse; ten camere occur in a length
of 10 mm. on the adoral part of the phragmocone. The camerz in-

crease orad in depth from .6 mm. to 1.5 mm, The living chamber

22, BULLETIN 103 62

has a ventral length of 16 mm. to the middle of the hyponomic
sinus which is broad and well developed. No trace of the si-
phuncle is retained. The surface bears rather coarse transverse
markings which retain the outline of the hyponomic sinus on the
venter.

Discussion.—This species is represented by two individuals in
the collection studied. In both, the phragmocone is filled with
calcite which is so extensively recrystallized that all internal
features are lost. The species is apparently a typical member of
the genus in form, but does not seem to be closely similar to either
of the previously described Ordovician species of North America.
R. carletonense Foerste is a larger and more rapidly expanding
form with coarser ornament. FR. coronatum Foerste and Savage
is more slender and is more comparable to FR. graciliforme de-
scribed above. The only other cephalopods of Rizoceras-like ap-
pearance in the Ordovician of America is an undescribed genus
and species of the Chazyan of New York which is orthochoanitic
and lacks a hyponomic sinus.

Types.—Univ. of Cincinnati, holotype, No. 22692, paratype,
No. 22693.

Occurrence.—From the Greendale member of the Cynthiana
limestone, at Cynthiana, Kentucky.

Family ONCOCERATIDZE
Genus NEUMATOCERAS Foerste

Genotype.—Neumatoceras gibberosum Foerste

This genus is a compressed exogastric cyrtoconic brevicone
clearly allied to Oncoceras and Beloitoceras from which it differs
mainly in its unusual form. The conch attains its maximum width
at a relatively early stage, after which it contracts laterally to the
aperture. While contracting laterally the greatest height of the
shell is attained, which is so strongly developed as to produce a
highly characteristic humped appearance. The ventral siphuncle
is described as being composed of slightly expanding segments.
The species -described below appears to be a typical member of
the genus in this respect. However, the only species for which

63 CYNTHIANA CEPHALOPODS: FLOWER 23

the siphuncle has been illustrated, N. nutans Foerste (1935, pl. 2,
fig. 1), shows a large orthochoanitic siphuncle instead.

The genus is developed in the Bighorn formation, the Fremont
limestone, and the Whitehead formation of Gaspé. Quite pos-
sibly Maelonoceras (?) reclinatum Troedsson (1926, p. 91, pl.
55, figs. 1-3) is a member of the genus, though a rather general-
ized one. It certainly lacks the adoral contraction over the adoral
surface of the living chamber figured for the genotype of Maelon-
oceras and shows no features inconsistent with regarding it as an
early Neuwmatoceras which is not as gibbous as are the younger
forms,

Neumatoceras carlsoni Flower, n. sp. Plate 3, figs. 3-5; Plate 4, fic. 9

Conch exogastric, cyrtoconic, compressed, the venter much
narrower than the dorsum. Venter uniformly curved adapically
with radius of curvature of 40 mm., becoming greater just before
attaining the living chamber and then nearly straight adorally.
The maximum width is attained about 5 mm. below the base of
the mature living chamber, where the width is 22 mm. Beyond
this point, the height increases for a short distance, while the
width steadily and gradually decreases to the aperture, so that
6 mm. farther, the width is 20 mm. and the height 23 mm ; in the
next 12 mm. the width becomes 16 mm. and the height 18 mm.

Seven camere are attached to the living chamber of the type.
The last three are considerably shortened. The sutures bear prom-
inent lateral lobes and rise farther orad on the venter than on the
dorsum. The siphuncle has a diameter of 2 mm. and is 2 mm.
from the venter. A fragment from the earlier part of the conch of
the same individual shows that the segments are relatively short
and broad, but are only very slightly expanded within the camere
and are empty. The living chamber is apparently not quite com-
plete ventrally, but the dorsal margin, which is straight, is clearly
preserved,

Discussion.—In form, this is a typical Newmatoceras, though
it is not as gibbous vertically as are some of the previously de-
scribed species. In this respect, it is somewhat closer to Beloit-
oceras, but in that genus the maximum height and width are
attained at about the same point, but the greatest shell height is

24 BULLETIN 103 _ 64

never found at a region where the conch is contracting laterally
orad.,
Type.—Holotype, Univ. of Cincinnati, No. 22694.
Occurrence—F rom the Greendale member of the Cynthiana
limestone, at Cynthiana, Kentucky.

Family OONOCERATIDZE
Genus OONOCERAS Hyatt
Genotype—Cyrtoceras lentigradum Barrande

Oonoceras Hyatt, 1884, Boston Soe. Nat. Hist., Proe., vol. 22, p. 280.

Ooceras Foord, 1884, Cat. Foss. Cephalopoda British Mus., vol. 1, p. 262.

Oonoceras Hyatt, 1894, Amer. Phil. Soc., Proc., vol. 32, pp. 447, 520.

Ooceras Hyatt, 1900, Cephalopods, in Zittel-Hastman 'lextb., Paleont.,
vol. 1, Ist ed., (Reprinted in later editions. )

Ooceras Ruedemann, 1906, New York State Mus., Bull. 90, p. 495.

ree Grabau and Shimer, 1910, North American Index Fossils, vol. 2,
p- 195.

mia See Foerste, 1926, Denison Univ. Bull., Sci. Lab., Jour., vol. 21,
p. 321.

Conch longiconic, cyrtoconic, only gently curved, compressed
in section with the venter more narrowly rounded than the dor-
sum and often subangulate. Expansion is very slow, and the ma-
ture part of the conch is essentially tubular. Sutures with slight
lateral lobes, the ventral saddles rising slightly higher than the
dorsal saddles. Siphuncle close to the venter, the segments very
slender in the genotype, being suborthochoanitic rather than
cyrtochoanitic. Species with broader segments are connected,
however, by intermediate types. The shell surface bears trans-
verse markings, normally thickened at intervals, sometimes simu-
lating the appearance of annuli as in the genotype. The surface
markings are not reflected upon the interior of the shell. A hypo-
nomic sinus is developed throughout life.

Discussion.—The early spelling of this name, Oonoceras, was
changed to Ooceras by Foord, a form which is consistent with
the proper usage of the original Greek. The early form of the
generic name is not to be regarded as a lapsus calamu (Knight,
1941). Although Hyatt (1900) subsequently recognized the
shorter form as correct and proposed the family Ooceratide, it
appears necessary to retain the original spelling.

The genus was first erected for slender compressed cyrtocera-
cones, but has come to be much more restricted in scope. Foerste

—

65 CYNTHIANA CEPHALOPODS: FLOWER 25

regarded Oonoceras (reéstablishing the original spelling) as char-
acterized by the development of annuli, a hyponomic sinus, and
a ventral empty siphuncle composed of slender segments. The
annulated appearance is more apparent than real. This is shown
by the absence of any trace of the “annuli” on the interior, and
also by the species, which show a transition between the geno-
type and forms with relatively smooth exteriors, marked only by
transverse lire and striz which are thickened at periodic inter-
vals. The ornament of the genotype represents only an extreme
development of the periodic thickening of the surface markings.
Foerste proposed the genus Oocerina, based upon Cyrtoceras
lentigradum Barrande, for species which differ from Oonoceras
in possessing broadly expanded siphuncular segments which are
occupied by actinosiphonate deposits.

Actually three groups are recognizable among the Silurian
species of Oonocevas and may be summarized as follows:

I. Forms with empty ventral siphuncles composed of
slender segments. Expansion is so slight within the camerz that
the condition is suborthochoanitic. The surface markings are
thickened at rhythmic intervals, often producing the effect of an-
nuli. This is to be regarded as Oonoceras, sensu stricto.

II. Forms with empty ventral siphuncles which differ from
the condition outlined above in being definitely cyrtochoanitic
and markedly expanded within the camere. The surface mark-
ings show the same thickening as in the above group, but are
usually less prominent. This group, although different enough in
siphuncular outline, does not seem to constitute a valid generic
group, inasmuch as it is connected with Oonoceras, sensu stricto,
by numerous species showing all gradations between the two types
of siphuncular outlines.

III. Forms with cyrtochoanitic ventral siphuncles which are’
occupied by actinosiphonate deposits. The surface features of the
type are not known; other species show surface markings similar
to those of the other two groups. Foerste regarded this group as
lacking a hyponomic sinus. While no sinus is figured for the
genotype, it is present in other species, and it is to be feared that
the drawing of the type is incorrectly restored at the region of

26 BULLETIN 103 66

the aperture. This is the group for which the generic name
Oocerina was proposed by Foerste.

There is reason to believe that Oocerina, itself, may not be as
distinct as a casual inspection of its features seems to indicate. It
is distinguished from certain species of group II only by the pres-
ence of actinosiphonate deposits in the siphuncle. Such deposits
have been used by Teichert as sufficient basis for the recognition
of the Actinosiphonata as a major group within the cyrotochoan-
itic nautiloids. However, enough is not known of the occurrence,
mode of growth, or function of these deposits to warrant their
use alone as a basis for the erection of major taxonomic groups.
The observations of the writer on Ordovician and Devonian
forms indicate that actinosiphonate deposits may be very erratic
in their occurrence. In some instances, they do not appear before
the gerontic stage of the individual and are absent in individuals
lacking such other indications of late maturity as the shallowing
of the adoral camerze and the development of incipient cameral
deposits in the phragmocone. In a Chazyan genus, soon to be
described, it was further noted that actinosiphonate deposits were
to be found only in the larger species; mature and gerontic in-
dividuals of the smaller species consistently lacked any trace of
the structures. The same has also been found to be true of the
Devonian genus Brezvicoceras, which can be traced to an origin
in actinosiphonate cephalopods of the Devonian and Upper Silur-
ian. This suggests that the puzzling condition found in the Chazy
genus is also not connected with the development of the deposits
in the large forms, but rather with the suppression of the struc-
tures in the small forms. Until more is known of the significance
of the structures, however, it is at least highly convenient to re-
tain Oocerina for the Oonoceras-like forms which possess actino-
siphonate deposits. It may eventually be shown that actinosipho-
nate forms are genetically distinct from nonactinosiphonate
cephalopods throughout the greater part of the Paleozoic. H,
however, the writer’s suggestion is correct that actinosiphonate
deposits represent the secretion of excess calcium carbonate in the
interstices of the siphonal vascular system, it 1s highly probable
that actinosiphonate deposits may have arisen independently in
many different genetic lines (Flower, 1938, p. 9; 1939, pp. 55-50).

67 CYNTHIANA CEPHALOPODS: FLOWER 27

Forms closely similar to the complex of Silurian species dis-
cussed above make up the dominant element in the fauna described
in the present paper. They are slender cyrtoceracones, unques-
tionably Oonoceras-like in form, and cannot be distinguished from
the species in group IT as outlined above, which are characterized
by broadly expanded siphuncles which lack actinosiphonate de-
posits. Closely related forms are found in the Ordovician of the
Arctic, in strata which have been variously regarded as Trenton
and Richmond. These include Oonoceras obstructum (Foerste,
1928, p. 307, pl. 52, figs. 2-3) of the Ordovician of Anticosti Is-
land, originally described as a species of Beloitoceras. Subsequent-
ly, relatively slender forms were separated as Richardsonoceras
Foerste, and related species from the Bighorn formation and the
Fremont limestone were described as Richardsonoceras wyom-
ingense Foerste and Richardsonoceras (?) subcuneatum Foerste,
(1935, pp. 40-42, pl. 3, fig. 1; pl. 7, figs. 3-4). Both appear to be
typical representatives not only of Oonoceras, but of the same
species group as that containing the Kentucky forms. Foerste and
Savage (1927, pp. 78-80, pl. 15, figs. 2-3) described two forms
from the Shamattawa limestone of Hudson Bay as Oocerina
shamattawense and Oocerina (?), sp. Neither is typical Oocerina,
but rather of the Ordovician species of Oonoceras.

In the Middle Ordovician there are no forms which are strik-
ingly similar to Oonoceras, but probably the ancestral radical is
found in typical Richardsonoceras Foerste (1933, p. 91). This
genus, based upon Cyrtoceras simplex Billings of the Black River
limestone of the Ottawa Valley, differs from group II of Oonoc-
eras mainly in superficial features ; nevertheless the types appear
to be very distinct in aspect and can be distinguished at a glance.
Oonoceras is very slightly curved, very slender, and has the septa
closely spaced and very flat. Richardsonoceras, on the other hand,
is more strongly curved, more rapidly expanding, and has rela-
tively distant septa which are not greatly flattened. In both
groups, the siphuncles are essentially similar; a hyponomic sinus
is developed. A difference of apparently minor importance 1s
found in the faint rhythmic recurrence of thickened surface mark-
ings on Ordovician Oonoceras. Although Richardsonoceras shells
are marked by fine transverse markings, periodic thickening of
the lines has not been noted.

28 BULLETIN 103 68

Richardsonoceras is known from the Black River and Trenton
of New York, southern Ontario, Wisconsin, and Minnesota.

Foerste has referred the following species to the genus:
Richardsonoceras clarkei Foerste, Black River of Wisconsin.
Richardsonoceras falx (Billings), Uppermost Black River,
Paquette Rapids, Ottawa River, Ontario.

Richardsonoceras romingeri Foerste, Black River, St.
Joseph Island, Lake Huron,

Richardsonoceras schofieldi (Clarke), Platteville, Wiscon-
sin.

Richardsonoceras simplex (Billings), Leray limestone of the
Ottawa Valley, Ontario.

Possibly Trenton species are related which have been referred
by Foerste to Cyrtorizoceras, but, as is shown below, generic
boundaries are dubious here also. These species appear to ex-
pand vertically too slowly to represent typical Cyrtorizoceras. As
the siphuncles are not known, it is possible, however, that they
represent the genus Paquettoceras Foerste, which is essentially a
smooth-shelled form of the orthochoanitic cyrtoconic genus Cen-
trocyrtoceras.

In attempting to carry Richardsonoceras farther back and to
connect it with related forms, difficulties of generic boundaries
are again encountered. There appears to be no fundamental dif-
ference between Richardsonoceras and Cyrtorizoceras, at least as
that genus is developed in the Ordovician, except the greater rate
of vertical expansion of Cyrtorizoceras. There are species which
might be placed in either genus with equal justification as far as
our knowledge of them extends at present.

Slender cyrtoceracones with uncontracted apertures, com-
pressed section, and cyrtochoanitic siphuncle are unknown in the
Chazy. However, related forms are known which differ only in
the slightly gibbous condition of the living chamber. These
species, forming a fairly uniform form group extending from the
Chazyan to the Richmond, constitute the genus Beloitoceras.
Some species very closely approach Richardsonoceras and also

4 In particular Cyrtorizoceras jfilosum (Conrad) of the Trenton and
Cyrtorizoceras camurum (Hall) of the basal Trenton, both of New York
See Foerste, 1928, pp. 186-189, pl. 42, figs. 3-4, ee

69 CYNTHIANA CEPHALOPODS: FLOWER 29

Cyrtorizoceras. A slight increase in gibbosity, located high on the
mature living chamber, produces the type of form diagnostic of
the much older genus Oncoceras, from which Beloitoceras was
separated for species of more generalized aspect. The form fails
to correlate with specific differences of the siphuncular out-
line between the two genera. This suggests strongly that
the genera are only form groups, and that actual genetic relation-
ships are probably more complex than the external form indicates.
Chazyan species are undeniably primitive, as is indicated by the
simple siphuncles which are suborthochoanitic at least in the early
stages. Most of these forms are in process of description by the
writer.

It has generally been considered that a contracted living cham-
ber is a phylogerontic condition, but the stratigraphic range of the
genera discussed entirely fails to support such a view. Instead,
Beloitoceras, with a faintly contracted living chamber, appears to
be the oldest member of this series so far recognized. No uni-
formly slender cyrtoceracones are yet known from the Chazyan
which might provide evidence of the antiquity of the supposedly
simpler type.

Beloitoceras varies in many ways, but variations in gibbosity
produce extreme types which have been separated as genera. In
Black River and Trenton times Oonoceras develops as an expres-
sion of extreme gibbosity, while more slender forms with parallel
sides or expanding living chambers constitute Maelonoceras, Cyr-
torigoceras and Richardsonoceras. Later on, variations within
Beloitoceras probably led to the development of the genera Win-
nipegoceras and Neumatoceras in the arctic faunas.

Richardsonoceras of the Black River-Trenton seas of eastern
North America probably gave rise to Oonoceras of the late-
Trenton and arctic faunas. This type appears to persist essen- |
tially unchanged into the Silurian of Bohemia, where form devia-
tion again occurs, producing the three form groups noted above,
which are based primarily on the variation of the siphuncular out-
line and structure. The further tracing of the history of this re-
markable complex is obscure. There is indication that Oxygont-
oceras is more probably related to Silurian Cyrtorizoceras, than

30 BULLETIN 103 70

Oocerina Lechritrochoceras

‘
4

’ :
, Oxygonioceras
,

octinosiphonote
SILURIAN
Oonoceras ll , ,Qonoceras | Cyrtorizoceras
XA chuncie ZZ

brood slender
Wr

RICHMOND

ARCTIC
Oonoceras || Digenuoceras Winnipegoceras

and
Neumatoceras

UPPER TRENTON ri
Beloitoceras

LOWER TRENTON
Cyrtorizoceras

Richardsonoceras Maplonoceras
CROCKLAND — HULL) Loganoceras

\ Beloitoceras

ae Monitoulinoceras << Oncoceras
compressed

BLACK RIVER Se a

Beloitoceras

Fig. 1. Diagrammatic representation of the development of Oonoceras and
its allies. Beloitoceras, the simplest of the Onecoceratide, appears in the
Chazyan. Variation in gibbosity results in a variety of forms ranging from
Oncoceras to Cyrtorizoceras, with the generic boundaries largely arbitrary.
Variation in section in nongibbous forms produces a similar range of gen-
era from the compressed Cyrtorizoceras and Richardsonoceras to the cir-
eular Loganoceras and the depressed Manitoulinoceras. Late Trenton to
Richmond types represent continuation of only a few of these genetic lines
and seem to lack the wide variation, form-genera being few in number and
fairly distinet. Wide variation in the form of the siphuncle again occurs
in the two divisions of the genus Oonoceras in the Silurian, while the de-
velopment of actinosiphonate deposits results in the genus Oocerina. The
relationship of Lechritrochoceras to Oonoceras, as indicated by the broken
line, is not thoroughly established. Oxygonioceras appears to be related to
Cyrtorizoceras on the basis of siphuncular structure. Many genera, largely
the relatives of Loganoceras and Manitoulinoceras, are omitted for the pur-
pose of simplification. In the present state of our knowledge, the most
startling break in the faunal record occurs in the middle of the Trenton,
making necessary the rather unusual grouping of the Ordovician strata
used here.

Vall CYNTHIANA CEPHALOPODS: FLOWER 31

to group II of Oonoceras. Further, it is probable that typical
Oonoceras gave rise to the costate trochoceroids which are par-
ticularly characteristic of the Silurian of both America and
Europe.

Further ramifications of form and section in the Ordovician
probably led to such genera of circular section as Loganoceras
and Kentlandoceras and to forms of depressed section of which
Manitoulinoceras is probably the best known example. While
there is considerable variation in the details of the siphuncular
outline of all of these Ordovician genera, all apparently agree in
having relatively small and usually slender siphuncles which are
ventrally located and devoid of any organic deposits. While it iS
not impossible that some forms, in particular those of depressed
section, may be connected to the ancestral radicle which gave
rise to the Mixochoanites upon the appearance of natural trunca-
tion, there is likewise no good structural basis for distinguishing
these forms from the evidently related compressed longiconic
forms of the Oncoceratide. The probable relationships within
this group are indicated in the accompanying diagram, which is
designed to emphasize particularly the dependence of the genera
on form,

Oonoceras planiseptatum Flower, n. sp. Plate 1, figs. 9-10; Plate 2, fig. 6

Conch compressed, with the venter only slightly more narrow-
ly rounded than the dorsum and with the greatest width occuring
at the middle of the section. The conch is slightly and uniformly
curved throughout the earlier portion, the radius of curvature
being 90 degrees, but it becomes straighter on the mature living
chamber, where the radius is increased to 110 degrees. The sec-
tion on the mature living chamber becomes more strongly com-
pressed. A phragmocone expands from 33 mm. and 37 mm. to
38 mm. and 44 mm. in a length of 45 mm. A complete living
chamber increases from 37 mm. and 43 mm., at the base, to 38
mm. and 47 mm., at the aperture, in a length of 35 mm.

The sutures are straight and transverse dorsally and dorso-
laterally. They slope slightly orad upon approaching the venter.
The septa are very flat, having a lateral curvature of 4 mm. where
the diameters are 33 mm. and 37 mm. The camere are very shal-

32 BULLETIN 103 72

low, sixteen to eighteen occurring in a length equal to an adoral
shell height of 44 mm. The siphuncle is not shown in any repre-
sentative of this species.

The aperture is slightly inclined orad from dorsum to venter
with reference to the plane of the last septum. The aperture is
straight dorsally and laterally, but shows indication of a hypo-
nomic sinus on the venter. The surface of the shell is not exposed.
The internal molds sometimes show longitudinal markings over
the phragmocone which represent incipient cameral deposits in
gerontic individuals.

Discussion.—From the slender rate of expansion, this species
must have attained a length of at least a foot when complete. Its
slender form distinguishes it from the only associated species
which attained comparable diameters. Other diagnostic features
are found in the dominantly transverse course of the sutures, the
very shallow camer, and the extreme compression of the mature
living chambers. The species is represented by only two good
specimens in our collection. One consists of a phragmocone of a
mature individual, the other is a living chamber which shows the
gerontic compression and reduction of curvature, but has not yet
attained the internal thickening of the shell wall.

T ypes.—Holotype, Univ. of Cincinnati Museum, No. 22680;
paratype, No. 22681.

Occurrence—From the Greendale limestone member of the
Cynthiana limestone, Middle Ordovician, at Cynthiana, Ky.

Oonoceras acutum Flower, n. sp. Plate 2, figs. 3-5

=H)

Conch only faintly curved, with radius of curvature for venter
120 degrees in the basal portion, but reduced adorally on the ma-
ture living chamber to about 90 degrees. The section is strongly
compressed, the venter subangulate. At the base, the height is
30 mm. and the width 25 mm. This increases at the base of the
living chamber to 29 mm. and 36 mm. in a length of 35 mm. The
living chamber has a maximum (dorsal) length of 37 mm. and
is incomplete adorally. It attains a width of 27 mm. and a height
of 37 mm.

The sutures slope slightly and uniformly orad from dorsum to
venter, but become slightly more inclined as the venter is ap-
proached. The camere are shallow, with a maximum depth of

73 CYNTHIANA CEPHALOPODS: FLOWER

3 mm., so that there are approximately fifteen in a length equal
to the adoral height of the shell. The siphuncle is located close
to the venter. The form of its segments has not been observed.
The living chamber is constricted internally on its dorsal side,
indicating that the type 1s a gerontic individual. The aperture is
not preserved. No trace of the original shell surface remains.
Discussion —The length of the living chamber of this form is
very similar to that of O. brevidomum, but the conch is uniformly
more slender, less rapidly expanding, and the diameters attained
are not so great. The extreme subtriangular form suggests O.
triangulatum, but, in addition to the larger size, the conch of this
species differs in being much more strongly compressed and in
possessing the region of greatest width well dorsad of the center
of the shell.
Types.——Holotype, Univ. of Cincinnati Museum, No, 22682;
paratype, Univ. of Cincinnati Museum, No. 22683.
Occurrence—From the Greendale member of the Cynthiana
limestone at Cynthiana, Kentucky.

Oonoceras (?) brevidomum Flower n. sp. Plate 2, figs. 1-2

This species is represented by a single crushed individual.
Though clearly related to the other species here placed in Oonoc-
eras, the general aspect of this form is rather that of a Beloitoceras.
In size, it approximates Oonoceras planiseptatum, but differs in
the more rapid expansion, the shorter living chamber and the
more oblique sutures. The specimen is 34 mm. high and 32 mm.
wide at the base and expands to 38 mm. and 46 mm., in a ventral
length of 38 mm, at the base of the living chamber. The living
chamber has a ventral length of 23 mm. and attains a height of
50 mm, and a width of 40 mm. The ventral outline is slightly
convex throughout, with an average radius of curvature of about
75 degrees. The dorsum is faintly concave. ,

The sutures are uniformly oblique, sloping orad strongly on
the venter. The camere are shallow, attaining a maximum depth
of 4 mm., while the earliest preserved camera has a depth Olv2
mm., and the last two are gerontically contracted. The siphuncle

is not preserved.

34 BULLETIN 103 74

The living chamber is short, the internal mold somewhat con-
stricted before attaining the aperture. The aperture is less cblique
than the last septum, straight dorsally and laterally and with a
small and not very sharply defined hyponomic sinus.

Discussion.—This species is easily confused only with O. plani-
septatum, which it most closely approximates in size. Even allow-
ing for the increase in rate of expansion, which might be pro-
duced vertically in the specimen by flattening, the rate of expan-
sion is obviously greater in this form, as is also the curvature.
In both features, the condition of Beloitoceras is approached.
More diagnostic are the markedly oblique sutures and the short-
ness of the living chamber.

Type.—Holotype, Univ. of Cincinnati Museum, No. 22684.

Occurrence.—From the Greendale member of the Cynthiana

limestone at Cynthiana, Kentucky.
Oonoceras multicameratum Flower, n. sp. Plate 3, figs. 1-2
Conch gently curved, radius of curvature of venter 100 mm.

over the mature portion. Section compressed, the venter more
broadly rounded than in O. graciliforme, and with greatest width
located at the center of the height, The shell expands from 21 mm.
and 23 mm. to 23 mm. and 25 mm. in the 22 mm. of the phragmo-
cone. In the 36 mm. of the living chamber, the height becomes
28 mm. and the width 24 mm.

The sutures bear slight lateral lobes, but are scarcely inclined
orad on the venter. The septa are very flat, having a maximum
depth of curvature at the base of the specimen of 3 mm, one-
seventh the width at that point. The camere are shallow, between
eleven and twelve occurring in a length equal to an adoral shell
height of 25 mm. The siphuncle is close to the venter. As ex-
posed at the apical end of the specimen, it has a diameter of 2.5
mm, and is slightly less than 2 mm. from the ventral wall of the
shell,

The surface is not preserved on any representative of this
species. The internal mold bears a dorsal constriction near the
adoral end of the living chamber found in no other species of this
association, but strongly reminiscent of Oonoceras obstructum
(Foerste) of the Vaureal limestone of Anticosti. The aperture is
not preserved except possibly on the extreme dorsal portion of
the shell.

75 CYNTHIANA CEPHALOPODS: FLOWER

wo
or

Discussion.—The shallow camere, nearly transverse sutures,
broader venter, and the development of the gerontic internal
thickening of the shell on the dorsum distinguish this from
O. gracilicurvatum. The rate of curvature is somewhat less in
this species, and the living chamber is slightly shorter in propor-
tion to its basal dimensions. A further difference is found in the
proportions of the living chamber, which is essentially parallel-
sided in O. graciliforme, but is faintly expanded in this species.
The gerontic constriction is found only on the dorsum of O. mutl-
ticameratum; in O. graciliforme it extends onto the venter.

Type.—Holotype, Univ. of Cincinnati Museum, No. 22685.

Occurrence.—From the Greendale member of the Cynthiana

limestone, at Cynthiana, Kentucky.
Oonoceras gracilicurvatum Flower, n. sp. Plate 4, fig. 3-5
Conch slender, slightly and uniformly curved, with radius of

curvature of venter 85 degrees. The section is compressed, with
the venter much narrower than the dorsum, the greatest width
lying scarcely dorsad of the center. The holotype expands from
22 mm. and 20 mm. to 25 mm. and 23 mm, in the 30 mm. of the
phragmocone. The living chamber has a ventral length of 45
mm. and at the apertural end measures 25 mm. and 23 mm. as at
the base. The aperture is not preserved. The internal mold is
constricted near the anterior end, indicating a gerontic condition,
also showing, by its position, that the living chamber was prob-
ably very nearly complete.

The sutures bear very shallow lateral lobes and are inclined
orad from dorsum to venter. Seven to eight camere occur in a
length equal to an adoral shell height of 23 mm. The last camere
show no evidence of gerontic shortening. The septa are not
clearly exposed, but are evidently very flat as in related species.
The siphuncle is located close to the venter and is cyrtochoanitic, |
apparently more broadly expanded transversely than vertically.
A segment 3 mm. long expands from 1.5 mm. to 3 mm. No trace
of deposits can be found in the siphuncle.

The shell wall is marked by numerous transverse strie and
lire which are rather irregularly thickened, giving the shell a
rugose appearance. On the venter, a well-developed hyponomic
sinus is indicated by these markings.

Discussion.—This is the smallest of the species of Oonoceras
in the fauna and may be further distinguished from its associates

36 BULLETIN 103 76

by the relatively deep camerze. The species which most closely
approximate this one in the proportion of the exterior of the shell
and in section differ in having shallower camere. Other minor
differences are found in the section of the conch and in the ex-
pression of the gerontic internal thickening of the shell near the
aperture. In this species a zone of thickening extends entirely
around the shell. In the preceding species it is found only on the
dorsum, as in the related Anticosti form, Oonoceras obstructum
( Foerste).

Type.—Holotype, Univ. of Cincinnati Museum, No. 22686.

Occurrence.—In the Greendale limestone member of the Cyn-
thiana, Middle Ordovician, at Cynthiana, Kentucky.

Oonoceras triangulatum Flower, n. sp. Plate 4, figs. 6-8

Conch slender and very gently curved, with radius of curvature
for venter of 105 degrees over the mature part of the shell. The
section is subtriangular, the venter subangulate, although the
greatest width of the shell is located scarcely dorsad of mid-
height.

The holotype retains 28 mm. of the phragmocone in which the
height increases from 20 mm. to 24 mm. and the width from 18
mm. to 21 mm. In the 42 mm. of the complete living chamber,
a height of 28 mm. and a width of 26 mm. are attained.

The sutures are slightly inclined orad from dorsum to venter
and bear very slight lateral lobes. Only the adoral two camer
are exposed. The last measures 2 mm. in depth, the preceding
one 3 mm. The siphuncle is not preserved on the specimen.

The aperture is not clearly preserved, and there is only an ob-
scure suggestion of a small hyponomic sinus. The surface bears
numerous fine alternating transverse lire and strie. At regular
intervals the lire are thickened, producing a costate aspect. The
coste are spaced from three to four mm. apart.

Discussion.—The subtriangular section, slender form, the poor
development of the lateral lobes, and the very slight curvature
serve to distinguish this species from all associated forms. It does
not appear to have any close relatives in other faunas.

‘Type.—Holotype, Univ. of Cincinnati Museum, No. 22687.

77 CYNTHIANA CEPHALOPODS: FLOWER 37

Occurrence.—In the Greendale member of the Cynthiana lime-
stone, at Cynthiana, Kentucky.

Oonoceras triangulatum var. cylindratum Flower, n. var. Plate 1, figs. 3-4

This form differs from O. triangulatum mainly in its much
more gradual rate of expansion. Radius of curvature of the venter
is about 105 degrees. The section is subtriangular, the dorsum
broad, the venter narrow and subangulate, though slightly broader
than typical triangulatum. The conch expands from 19 mm. and
21 mm. to 22 mm. and 25 mm. in 35 mm. in the earliest stage
represented. In the holotype, the phragmocone shows an increase
from 21 mm. and 24 mm. to 25 mm, and 29 mm. in 30 mm., while
the living chamber changes in 45 mm. to 29 mm. amc 27 madi) AN
second living chamber shows almost identical proportions.

The sutures are somewhat oblique and bear slight lateral lobes
and agree essentially with those of typical triangulatum. The
camere occur between ten and twelve in a length equal to an
adoral height of the shell. The siphuncle is very close to the
venter, measuring 3 mm. in diameter as exposed at the base of
the holotype, and 1 mm. from the venter.

The shell surface is marked by faintly rugose transverse stria
and lire, somewhat less strongly developed than in O. gracili-
curvatum. The aperture is not clearly preserved in any specimen,
but the lines of growth show the development of a well-defined
hyponomic sinus on the venter.

Discussion.—This form differs from O. triangulatum mainly in
the less rapid expansion. The curvature of the venter of the two
species and the size and proportions of the living chamber are
very similar, as is the depth of the camere. The venter is slightly
more rounded in this form. It is not impossible that the differ-
ences involved might represent sexual dimorphism, but the pres-
ent material is not adequate to warrant any definite conclusion on
this subject.

Types —Holotype, No. 22688, paratypes, Nos. 22689, 22690,
University of Cincinnati Museum.

Occurrence-—From the Greendale limestone member of the
Cynthiana, at Cynthiana, Kentucky.

38 BULLETIN 103 78

Oonoceras suborthoforme Flower, n. sp. Plate Wen fie. ele
A fragment of a phragmocone with a maximum length of 24

mm. represents still another species of Oonoceras. Curvature is so
slight that the lateral view is hardly sufficient to determine that
the venter is located at the left side as the specimen is oriented in
our illustration. The section is scarcely higher than wide, the
greatest width, however, occuring slightly dorsad of the center so
that the venter is very slightly more narrowly rounded than the
dorsum. The conch expands from 20 mm. and 19.5 mm. to 23
mm. and. 22.5 mm., in the length of 25, mm: The sutures hear
prominent lateral lobes, but rise adorally about equally on dorsum
and venter. Nine camerz occur in the length of 20 mm. The
adoral camere are slightly shallower than the others, suggestive
of the approach of a gerontic condition. The siphuncle is close
to the venter, but is not clearly marked. The specimen is remark-
able for the development of a series of grooves upon one side of
the internal mold. They represent molds of cameral deposits not
elsewhere preserved on the conch; they have not been noted in
other species of the genus. The surface, living chamber, and
aperture are unknown.

Discussion—In spite of the fragmentary nature of the type this
form may be readily recognized by the straight condition of the
shell and the marked development of lateral lobes which is not
accompanied, as is usual in the genus, by the development of
oblique sutures extending farther orad on the venter than on the
dorsum.

Type.—Holotype, Univ. of Cincinnati Museum, No. 22762.

Occurrence.—From the Greendale member of the Cynthiana
limestone, from Cynthiana, Kentucky.

Family DIESTOCERATID®

Genus DIESTOCERAS Foerste
Diestoceras ? sp. Plate 1, figs. 5-6
Among the material from the Cynthiana lens are fragments of
a moderately large breviconic form which appears to fall in the
genus Diestoceras on the basis of the compressed section, slight
contraction of the shell near the aperture, the straight and trans-
verse sutures and the scalariform siphuncle. Three specimens of

79 CYNTHIANA GEPHALOPODS: FLOWER 39

this form were encountered, but all of them contained a geodic
filling of coarse calcite crystals in the living chamber making suit-
able extraction impossible. The phragmocone of the best pre-
served individual is compressed throughout, having a basal width
of 22 mm., a basal height of 24 mm., increasing in 37 mm. to a
width of 37 mm. and a height of 40 mm. The venter is slightly
convex, the dorsum is straight. The sutures are straight and
transverse. The camer average 2 mm. in depth, with variation
of less than .5 mm. in the known portion of the phragmocone.
The siphuncle lies close to the venter. A segment, 2 mm. long,
has a diameter at the septal foramen of .7 mm., and expands to
2.2 mm. In vertical outline the segment is scalariform, being
adnate dorsally on the adoral end and ventrally on the adapical
end. No trace of organic deposits is preserved in the camere.

The living chamber is known only from inadequate fragments.
The largest fragment of a living chamber has a height of 50 mm.
and a width of 46 mm. In this specimen there is no definite trace
of apertural contraction, though this has been observed in a lateral
fragment of a slightly larger individual.

Discussion.—The rapid rate of expansion of the phragmocone
distinguishes this from the associated species of Oonoceras, from
which it is further distinguished by the scalariform outline and
broadly expanded condition of the siphuncular segments. Enough
is not known to make possible any close comparison with the de-
scribed species referred to Diestoceras. The preservation may in
part account for the absence of actinosiphonate deposits in the one
siphuncle sectioned; it is also true that this is an immature in-
dividual, as shown by the lack of evidence of adoral contraction
of the shell and by the absence of adoral shallow camerz and also
by the absence of the longitudinal markings on the internal mold
of the phragmocone generally present in mature individuals of
this genus.

Type.—Univ. of Cincinnati Museum, No. 22699.

Occurrence.—From the Greendale member of the Cynthiana
limestone (Trenton), at Cynthiana, Kentucky.

40, BULLETIN 103 80

REEPERENCES

Dunn, P.
Geological map of Harrison County, Kentucky, Kentucky Geol.
Surv., ser. 6, 1930.

Flower, R. H.
Devonian brevicones of New York and adjacent areas,
Paleontographica Americana, vol. 2, No. 9, 1938, 84 pp., 4 pls.,
10 figs.

———— Study of the Pseudorthoceratide, Paleontographica Americana,
vol. 2, No. 10, 1939, 214 pp., 9 pls., 22 figs.

» Some Devonian Actinoceroidea, Jour. Paleont., vol. 14, 1940,
pp. 442-446, pl. 61.

Flower, R. H., and Caster, K. E.
The stratigraphy and paleon‘ology of northwestern Pennsyl-
vania. Part IJ, Paleontology. See. A: The cephalopod fauna
of the Conewango series of the upper Devonian of New York
and Pennsylvania, Bull. Amer. Paleont., vol. 22, No. 75, 1935.

Foerste, A. F.
Preliminary notes on Cincinnatian fossils, Denison Univ. Bull.,
Sei. Lab., Jour., vol. 14, 1909, pp. 209-232, pl. 4.

————— Preliminary notes on Cincinnatian and Lexington fossils,
Denison Univ. Bull., Sci. Lab., Jour., vol. 16, 1910, pp. 17-100,
pls. 1-6.

———— Cephalopoda, in Twenhofel, Geology of Anticosti Island, Can-
ada Geol. Surv., Mem. 154, 1928, 480 pp., 60 pls.

———§— Black River and other cephalopods from Minnesota, Wisconsin,
Michigan and Ontario, Part I, Denison Uniy. Bull., Sci. Lab.,
Jour., vol. 27, 1932, pp. 47-136, pls. 7-37.

——— Black River and other cephalopods from Minnesota, Wisconsin,
Michigan and Ontario, Part II, Denison Univ. Bull., Sei. Lab.,
Jour., vol. 28, 1933, pp. 1-146.

——— Bighorn and related cephalopods, Denison Univ. Bull., Sei.
Lab., Jour., 1935, pp. 1-96, pls. 1-22.

———— Cephalopods from the Upper Ordovician of Percé, Quebec,
Jour. Paleont., vol. 10; 1936, pp. 373-384, pls. 54-57.

———— Cephalopoda in Twenhofel, Geology and paleontology of the
Mingan Islands, Quebec, Geol. Soc. Amer., Special Paper, No.
11, 1938, pp. 76-105, 24 pls.

Foerste, A. F., and Savage, T. E.
Ordovician and Silurian cephalopods of the Hudson Bay area,
Denison Univ. Bull., Sci. Lab., Jour., vol. 22, 1927, pp. 1-108,
pls. 1-24.

Foerste, A. F., and Teichert, C.
The actinoceroids of east-central North America, Denison
Univ. Bull., Sci. Lab., Jour., vol. 25, 1930, pp. 201-296, pls.
27-59.

Hyatt, A.
Cephalopoda, in Zittel-Eastman Textbook of Paleontology,
vol. 1, 1st ed., 1900, pp. 502-595. (Reprinted, 2d edition, 1913,
pp. 583-616.)

81 CYNTHIANA CEPHALOPODS: FLOWER 41

Kay, G. M.
Ordovician Stewartville-Dubuque problems, Jour. Geology, vol.
43, 1935, pp. 561-590, 10 figs.

Knight, J. B.
Are corrections to the original spelling of generic names ad-
vantageous? Amer. Jour. Sci., vol. 239, 1941, pp. 312-315.

McFarlan, A. C.
Stratigraphic relationships of Lexington, Perryville and Cyn-
thiana (Trenton) rocks of central Kentucky, Geol. Soc. Amer.
Bull., vol. 49, 1938, pp. 986-996, 1 pl., 1 fig.

Miller, A. K., Dunbar, C. O., and Condra, G. E.
The nautiloid cephalopods of the Pennsylvanian system in the
mid-continent region, Nebraska Geol. Surv., ser. 2, Bull. 9,
1933, 240 pp., 24 pls., 32 figs.

Ruedemann, R.

The Utica and Lorraine formations of New York. Part Il,
Systematic paleontology, No. 2, Molluscs, crustaceans and
eurypterids, New York State Museum Bull. 272, 1926.

Shimizu, S., and Obata, T.
Three new genera of Ordovician nautiloids belonging to the
Wutinoceratide (nov.) from east Asia, Jour. Shanghai, Sci.
Inst., sec. 2, vol. 2, 1936, pp. 27-35.

Teichert, C.
Untersuchungen an actinoceroiden Cephalopoden aus Nord-
gronland, Medelelser om Grénland, Bd. 92, Nr. 10, 1934, pp.
1-48, 22 figs.

Troedsson, G. T.
On the middle and upper Ordovician faunas of northern Green-
land, I, Cephalopods, Meddelelser om Gronland, Bd. 71, 1926,
pp. 1-157, pls. 1-65.

Ue a os ¥ qeH a ea ety By ye

Ona oo I i
ae racine) per vm ra ities ee :
saa -_ “wih os = Oe yy ood x

Viobee * i mi ep Real «tf

Das ssi ‘anes ir Ata Supp ee dttey Ai ie, snohaliasiny, oth,
fe ESS on ah ie He sik ie ee 0% Aer, Seen bnby

vita ~ Ket: ree ry waid neh) vet atlas dat ab gente
volte & Mes ite? hehcvos) Verse “ely iw ko (notion } WHHL
‘ nee wah 2) why Ky ieoeitigtt “hy LOG te icy: biti. an
| : .) 2 dab? bes LO .0, dedaod A
ay eh OY vat an Ts rarest ast Se Srerwgtel sais ay BYE Brat aie
® io of MSN (crit iO evade notin Laniies- Bia! |
foe i eis mn og Me Be ae oa ae th eaeetcits &

ea

If fon Ait wun LGUKTRAWOT. 3 ivan Bis Ror} one
Roney sy REBT ES * ae ee mee day Nay ha) SST”
VSO eSe ited capers se Foe ae: | rat ch se meivandened os ;
. ‘ va Pe Me TP” teh Brees a
MAT OF werywola ah) sheind cmiatpabiy Ws Wishaw Sota

se}. caagte! fet “aio eR Pens ata boa ahhirtaves Mya :
= Ad BE. ve acy pon LS loo See yaeile

-bie. sity nebogoliniqad cablowsotiign wey jeans
eg fel Eb na See et be role 1) to awels foheit Sylar -
i ae Ce aia . ae 4) ORM SS ake k
= , ‘ a ures?
) | =e eS AIG Lay BAM, alate dy) r sum Sao, Shahn Bab a,
HeeE FF be dhomabedo 4 toh roefslonh ehh abeyakniacs YL. Ssh:
A) ary © : = Gh. [ BN Vell ALT

Dnrraaiget |

ty ee

44 BULLETIN 108

EXPLANATION OF PLATE I (4)

84

Figure Page

1. Treptoceras perseptatum Flower, n. sp. een!
Horizontal section of holotype, Univ. of Cincinnati, No. 22679.

2} Dreptoceras prenuntiums blower, i. |S). ————
Horizontal section of holotype, Univ. of Cincinnati, No.
22696.

3-4. Oonoceras triangulatum var. cylindratum Flower, n. sp. __- 2
Paratype, (3) left lateral and (4) dorsal aspects. Univ. of
Cincinnati, No. 22690.

5-6. Diestoceras ? sp. :
(5) Ventral aspect of fragment: wy “phragmocone @ vertical
section of the same specimen. Univ. of Cincinnati, No.

22699

Sh UZ OCCEAS eC OMLCUTTIE EO) WiC sminn eS [ae ee ee
Holotype, (7) ventral and (8) left lateral aspects. Univ.
of Cincinnati, No. 22691. ’

9-10. Ocnoceras planiseptatum Flower, n. sp. —— i
Holotype, (9) dorsal (10) right lateral: ‘aspects. “Univ. of
Cineinnati, No. 22680.

11. Oonoceras suborthoforme Flower, n. sp. —-— :
Holotype, left lateral aspect, showing unusual ‘development
of longitudinal furrows on internal mold representing cam-

erai deposits. Univ. of Cincinnati, No. 22762.

All specimens are from a lens in the Greendale member of the Cyn-
thiana limestone, Middle Ordovician, from the Poindexter quarry, Cyn-
thiana, Kentueky. Illustrations natural size.

37

38

21

31

38

Pu. 4, VOL. 27 Buu. AMER. PALEONT. No. 103, Pu. 1

PLATE 2 (s)

46 BULLETIN 103 86

EXPLANATION OF PLATE 2 (5)

Figure Page

1-2. Qonoceras brevidomum Flower, n. sp. —~ -—~. .-~ - = 33
Holotype, (1) left lateral and (2) dorsal views. ‘Univ. of
Cincinnati, No. 22684.

3-5. Oonoceras acutum Flower, n. sp. Jena2
Holotype, (3) left lateral (4) dorsal and (5) septate views.
Univ. of Cincinnati, No. 22682.

6. Oonoceras planiseptatum Flower, n. sp. . poco
Paratype, septal view. Univ. of Cincinnati, No. 22681.

7. Rizoceras graciliforme Flower, n. sp. = eeo le ene
Holotype, lateral aspect, venter on “right. Univ. of Cinein-
nati, No. 22693.

All specimens are from a lens in the Greendale member of the Cyn-
thiana limestone from the Poindexter quarry, Cynthiana, Kentucky.
Illustrations natural size.

Pi. 5, VOL. 27 Buu. AMER. PALEONT. No. 103, Pu. 2

“Mort Wu worravzasaxcl

,
as
5

eit
D oa seat Tt pistovoning isin satiqpmad) Sok
vie why Lau iti is $4 } ; + Peta th ST BL Lo 6 4 eoet ysuloH

= ainhi
sVONSS 3)

fl tnashtso aetes ote

Pees 0 va ia ts }

a

ab Ente 2 os

yse
1

Oye doa sodiroear ol piney

emo TL sede,

48 BULLETIN 105 88

EXPLANATION OF PLATE 3 (6)

Figure Page

1-2. Oonoceras muiticameratum Flower, n. sp. — . 2
Holotype, (1) Ben lateral and (2) dorsal aspects. “Univ. of
Cineinnati, No. 22685.

3-5. Neumatoceras carlsoni Flower, n. sp. ss 23
Holotype, (3) ventral, (4) right lateral ‘and (5) dorsal. ‘Univ.
of Cincinnati, No. 22694.

6. Treptoceras perseptatum Flower, n. sp. ~~~ — 1 18
Paratype, Univ. of Cincinnati, No. 22698,

7-8. Oonoceras triangulatum var. cylindratum Flower, n. sp. -<o SOM
Holotype, (7) ventral and (8) lateral aspects. Univ. of
Cincinnati, No. 22688.

9. Oonoceras planiseptatum Flower, n. sp. ~ : =: eo
Holotype, dorsal aspect. Univ. of Cine innati, No. 22680.

All specimens are from a single lens in the Greendale member of the
Cynthiana limestene, from the Poindexter quarry, Cynthiana, Kentucky.
Illustrations natural size.

PL. 6, VOL. 27 Buuu. AMER. PALEONT. No. 103, PL. 3

PLATE 4 (7)

50 BULLETIN 103

EXPLANATION OF PLATE 4 (7)

90)

Figure Page
1-2. Treptoceras persiphonatum Flower, n. sp. 17
Holotype, (1) exterior of phragmocone (2) horizontal see-
tion. Univ. of Cincinnati, No. 22695,
35

3-5. Oonoceras gracilicurvatum Flower, n. sp.
Holotype, (3) ventral aspect (4) lateral aspect (5) dorsal
aspect. Univ. of Cincinnati, No. 22686.

6-8. Oonoceras triangulatum Flower, n. sp.
Holotype, (6) ventral (7) right lateral (8) dorsal aspect.
Univ. of Cincinnati, No. 22687.

9. Neumatoceras carlsoni Flower, n. sp. -
Holotype, vertical section of portion of phragmocone. Univ.

of Cineinnati, No. 22694.

All specimens are from a lens in the Greendale member of the Cyn-
thiana limestone, Middle Ordovician, from the Poindexter quarry,
Cynthiana, Kentucky. Illustrations natural size.

36

23

Pu. 7, Vou. 27 Buu. AMER. PALEONT. No. 103, Pu. 4

Po CUNGHe Oa n Jamal 4: Ds! SU DIS. ee ls ene Ea Se Lun Pah NG 6.00
Mainly WBecuadoran, Peruvian and Mexican Tertiary
forams and mollusks and Paleozoic fossils.
Va UINOSOdAOL) a) AOD 4s) PIS see wel Ss Ll ee 5,00
Venezuela and Trinidad Tertiary Mollusca.
ROVE NONOH:; 02-03 )a 7h 26, DD. hos) PlSsia eee Seat SN a 6.00
Peruvian Tertiary Mollusca.
SVR CN ONS =G4=67,) 272565. DIP) 29 Diss a ea td Ee en 6.00
Mainly Tertiary Mollusca and Cretaceous corals.
eer ON GOS Lee ID ic AAD Bae 2 sete) Pn 2 eae I Se 5.00
Tertiary Paleontology, Peru.
Se Re NGS Oo =F 0C) 2! AGO. Dawa Ou PIS, + ee Non nee he pie 6.00
Soy Cretaceous and Tertiary Paleontology of peru and Cuba.
MM UNOSsidmde ye cool ipps Amipis: wt Ale er oe a, 5.00
sy Paleozoic Paleontology and Stratigraphy,
ia emiien (NOR Gta tG) S0Gt Dpe ot piss ss ok Uke aes ie 7.00
Paleozoic Paleontology and Tertiary Foraminifera.
Reet NOB srs ado) = oD: DPS Oo PIS. ys ee ee ee 5.00
Corals, Cretaceous microfauna and Se ra ‘Conrad:
XXIV. (Nos. 80-87). 334 pp., 27 pls. ee eA GLOU,
Mainly Paleozoic faunas and Tertiary Mollusca.
XXV. (Nos. 88-94B). 306 pp., 30 pls. 2 | She coe aN et OU
Paleozoic fossils of Ontario, Oklahoma and Colombia,
Mesozoic echinoids, California Pleistocene and Maryland
Miocene mollusks.

mewn cONOS: 9u-100)- 420 cp pis DS. splsa arn tae ee OU I ns 7.00
Florida Recent marine shells, Texas Cretaceous fossils,
Cuban Cretaceous corals, and geology and paleontology
of Ecuador.
Cuban and Peruvian Cretaceous, and Peruvian Eogene
corals, and geology and paleontology of Ecuador.
XXVII. (Nos. 101-103, other numbers in preparation). 90 pp. 7pls. 2.00
San Pedro, California Pleistocene Mollusca and early

ati stb

° aa

ek SE ee
ah Soars - ee

ir burned
a

4 Paleozic cephalopods from Alaska and Kentucky.

:

: PALASONTOGRAPHICA AMERICANA

; Volume I. (Nos. 1-5). 519 pp., 75 pls. _... $12.00
, Monographs of areas, Lutetia, rudistids ‘ard venerids.

Volume II No’s 6- 12— ST eee earns 2 Le Eae $12.00

rie a*

Volume III. (No. 13, other numbers in preparation). 56 pp. 3 pls. .. 1.25
Eurysiphonate cephalopod structure and phylogeny.

. ae Paleontological Research Institution

Ithaca, New York
ie Maes:

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 104

Type Fossil Cypreide of North America

By

William Marcus Ingram
Mills College, California

August 11, 1942

Paleontological Research Institution
Ithaca, New York
WEF Ssn.

LipRAn

MN hb.
JP OTOON CMOCG BLN:
COA BR OOTAOM Aa

CONTENTS

MV erartays OC Citsd OT eeeee taea aek eyo eee SO Seese neta Sea em ee een eee ee aoe
Clnssifcation? of the Cypirmeide considered: 2:22.22 s eaves seer
General discussion -..-............... Seabee WE 5h 58 ee eee eA Nr 9 Se
Age of Cypreide .....:. eR ae ace an Se eee ea en a Oe
june iclationsiips between fossil and Keeent Cypreide of the
WC SGI N eA EL CTL STC 1 Cia tree oie coe se oon ees eee ne = ee eee eee
INOMEXIStCM i ACOLMISS wh se. 5 te Fel 2? 2. pe Ee erent eee Ee a bee
ANN KOON] G CLO GIN GS seen ee hse kB Eres ee ee Saco eae Senne san, cco en
List of type fossil Cypreide of North America ._..__......0......222.2-----
Cypraa occurring in both the fossil and living state in North
ANTOTTTEYOY, SE 5 EEO aoe EY Rae tne ean oye re Oo ey nee eee, eae
ID anal asereul:: (Ohi orgeenyele eg See Sores oe ee a cue Re ue a gan ey ee eee
TET SUIT yma OU TI ged A DA ele SR ae Dy em as erga ee ee

JOE HASY <Resk lay pula UNeg a Otel ae ee ROR E aes Os nA D fee ALE ear eres ees PORRE AE

TYPE FOSSIL CYPRAAIDAY OF NORTH AMERICA
By
WILt1AM Marcus INGRAM
Mills College, California

INTRODUCTION

This paper is a product of an attempt to gather information
dealing with holotypes of .the fossil Cypreide of North
America. Many holotype numbers and holotype depositories are
here listed for the first time. Type localities are included and
the geological age of the holotypes is cited. The first illustrations
of many of the holotypes by the photographic method
are included. Questions which have been referred to the writer
concerning the above points have prompted a publication of such
a paper.

No worker has yet attempted to make such a survey, Schilder
(1932) published a list including many of the forms which come
within the scope of this paper, but he made no attempt to include
information about holotypes. He had no opportunity to examine
the many type specimens housed in the United States, and, from
erroneous data included in his “Fossilium Catalogus,” he has not
studied many of the species included here. Vredenburg (1920)
listed a number of fossil species from localities in North America
in his interesting consideration of the classification and antiquity
of the Cypreide. His work, though not complete, is a world-
wide, general consideration of this group, with great emphasis
placed upon systematic relationships of many species. Schilder
(1926), who later examined and corrected Vredenburg’s (1920)
work, included relative data concerning some of the species dealt
with here.

The writer believes that the Cypreeidz included here represent a
fairly complete assemblage of the species described from North
America, although some species may have been unavoidably over-

looked.

6 BULLETIN 104 96

GLUASSIPICATION OF DHE CY PRADA
CONSIDERED

Five genera are recognized here as belonging to the North
American Cypreide. These are: Cyprea Linneus, Cypredia
Swainson, Sulcocyprea Conrad, Siphocyprea Heilprin and Gisor-
tia Jousseaume. The greatest number of species is assigned to
the genus Cyprea. The writer has not attempted to subdivide
the Linnean genus Cyprea further, believing that it is best to wait
until anatomical relationships of Recent forms are known and
can serve as a possible guide in correlating fossil affinities. Num-
erous European writers, notably Schilder,) have attempted to
divide the original genus Cyprea into innumerable genera that
intergrade one into the other. The genera recognized here are
natural ones ; they show no intergradations from one to the other.
The variability in the family Cypreide and intergradations of
generic characteristics in this group are well known by one who
has studied them to even a small extent; many of the characters
used to separate the so-called genera seem to be relative and not
specific. In this connection it is well to quote Sowerby (1870)
in his reference to living species.

In aitempting to arrange the Cyprea in groups according to their affini-
ties, it is difficult to find any leading principle of association or separation,
because shells associated by one set of characters are disassociated by
others. Thus, C. capensis and C. Adamsonii have been placed by some
authors under the name ‘‘ Cypreaovulum’’ on account of their resemblance
in their system of dorsal striation, but in all other characters their affini-
ties are widely apart.

Neither can the species be well separated according to their general
forms, or the degree of thickening of their sides by superdeposited enamel,
because, in these respects, the species pass from one to the other by imper-
ceptible gradations, and because widely different forms are found in the
same species. Thus, the common short C. carneola, with thickened sides,
would, in arrangement depending upon forms or lateral expansion, be
placed in a group with C. arenosa, which it greatly resembles, while the

cylindrical form of the same species would range with C. testudinaria and
C. argus.

top. Ct.

97 Cypraipa or NortH AMERICA: INGRAM 7

GENERAL DISCUSSION

Certain of the genera of Cypreeidz are restricted in their strati-
graphic ranges. The genus Cypredia, represented in North
America by three species, is confined to the Eocene, and all have
limited geographic ranges. Two species, Cypredia gilberti
Palmer and Cypredia subcancellata (Johnson) are from the Clai-
borne, middle Eocene; the former species was described from the
Gosport sand, Monroe County, Alabama, and the latter from thé
Claiborne Eocene of Smithville, Bastrop County, Texas. Cypre-
dia fenestralis (Conrad) is from the Jackson, upper Eocene of
Jackson, Mississippi. Olsson (1931) described a Cypredia chira
from the lower Oligocene, Peru. This occurrence seems to be
the only one in the South and Central American area. Trech-
mann (1923) described Cypredia elegans (Trechmann), and
listed Cypredia elegans (Defrance) from the ‘Yellow limestone”
of Jamaica, which probably represents a middle Eocene occur-
ence. Schilder (1939) described Cypredia vistabellensis and
Cypredia kugleri from the upper Eocene of Trinidad. With the
exception of Olsson’s (1931) species, the Cypredia in our hem-
isphere are of Eocene occurrence.

The genus Sulcocyprea Conrad, represented at this time by
only the genotype, Sulcocyprea lintea (Conrad), is confined to
North America, occuring in the Jackson Eocene and Vicksburg
Oligocene in Mississippi. Schilder (1932), disregarding the
characters of the genotype, erroneously placed numerous North
American species in this genus.

Stphocyprea Heilprin occurs exclusively in the Pliocene of
Florida, and is represented only by its genotype, Siphocyprea
problematica Heilprin. Schilder (1932) incorrectly included
other hemispheric species of Cypreide in this genus, 7. e.,
Cyprea amandusi Hertlein and Jordan, Cyprea henekeni Sower-*
by, Cyprea mus Linneus, Cyprea carolinensis Conrad, ete.

Only one specimen of the genus Gisortia has been collected in
North America. Reference to this specimen was first published
by Clark and Vokes (1936) ; it was described by Ingram (1940)
as Gisortia clarki, from the Capay stage, Llajas formation, lower
zone, Simi Valley, Ventura County, California.

BULLETIN 104 98

ive)

The genus Cyprea is the most widely distributed in the fossil
record, extending from the Cretaceous through Pleistocene and
Recent. Geographically, fossil species extend from coast to coast
in North America. Thirty-three species and subspecies of
Cyprea are found in the fossil state in North America.

AGE OF CYPRAZIDZ.

Present data would indicate that the Cypreide had a Jurassic
or possibly even an earlier origin. At that time the center of dis-
persal seems to have been in Europe; the two Jurassic occur-
rences are from the Tithon stage in Sicily. The two species,
Cyprea gemmellaroi and Cyprea tithonica, were described by
Stefano (1882). If available stratigraphic records are reliable,
data included here would indicate that a radiation from this pos-
sible Jurassic center of origin soon occurred, since three so-re-
ported Cretaceous species, Cyprea suctensis Whiteaves? from
British Columbia, Cyprea squyeri Campbell from Montana and
Cyprea mortoni Gabb? from New Jersey, are found in North
America, Since the peak of production of numbers of species
occurred in the Eocene of North America, it is possible to assume
that the Cypreidz were well established and on a decline before
the family was well established in the West Indies and South and
Central America, where the maximum number of species thus
far reported are of Miocene occurrence.

SOME RELATIONSHIPS BETWEEN FOSSIL AND
RECENT CYPRAIDAZ OF THE WESTERN
HEMISPHERE

This section discusses generally the relationships between
some of the living and fossil species of the Western Hemisphere.
A number of included species do not occur in fossil or living
states in North America, but the discussion seems pertinent since
some of the South and Central American and neighboring island
species are related to the North American Cypreide.

2 Although these ‘‘species’’ possibly belong to the Cypreide, their
generic rank is doubtful (see text).

99 CyPR2XID& OF NortH AMERICA: INGRAM 9

Ten species, found as fossils in the Western Hemisphere, are
still present in the living state. Three fossil species have traceable
living descendants. The former species are Cyprea spurca Lin-
neus, Cyprea spadicea Swainson, Cyprea cinerea Gmelin,
Cyprea arabicula Lamarck, Cyprea sowerbyi Kiener, Cyprea
albuginosa Mawe, and Cyprea isabella Linneus, Cyprea nigro-
punctata Gray, Cyprea cervinetta Kiener, and Cyprea cervus
Linneus. The latter species are Nuclearia gabbiana (Guppy),
Cyprea trinitatensis Mansfield, and Cyprea henekeni Sowerby.

Nuclearia gabbiana (Guppy) has been reported by Maury
(1917) and listed by Ingram (1939e) from the lower Miocene
of Santo Domingo. It has a Miocene occurrence in Haiti, Trim-
dad, and Columbia. A living representative is the Indo-Pacific
species, Nuclearia nucleus (Linneus). This latter species is now
abundantly found throughout the tropical and temperate waters
of the Pacific. A probable descendant of N. nucleus in the
Hawaiian Islands is N. madagascariensis (Gmelin), Ostergaard
(1928), Ingram (1939d). Available fossil evidence thus indi-
cates that the Santo Domingo area was possibly the center of
origin for the present-day widely distributed N. nucleus (Lin-
nzus ).

The possible living descendants of Cyprea trinitatensis Mans-
field are Cyprea cervinetta Kiener, Cyprea zebra Linneus, and
Cyprea cervus Linneus. These species have a restricted Western
Hemisphere distribution. In the fossil state C. trinitatensis has
been reported from the lower Miocene of Trinidad.

Cyprea mus Linnzus is no doubt a living descendant of the
Miocene “Cyprea henekent group.” This cowry group, made up
of closely related forms, seems to have been the most widely
spread of any Cypreidze in Miocene time. Cyprea henekent
Sowerby has been reported from the Miocene of Santo Domingo
by Maury (1925). The writer has examined specimens from the
Miocene of Costa Rica and Panama. Other fossil forms of the
Western Hemisphere which are closely related to the living
Cyprea mus are: C. henekeni var. poteronis Ingram and C. noulei
Maury from the Miocene of Santo Domingo, C. merriami Ingram
from the Miocene of Panama, C. henekent amandusi Hertlein and
Jordan from the Miocene of Lower California, and Cyprea

10 BULLETIN 104 100

cayapa Pilsbry and Olsson from the Pliocene of Ecuador. Con-
cerning the holotype of C. cayapa, Pilsbry and Olsson (1914)
state: “Before being entombed in the sediments, the shell had been
eaten into by boring organisms and partly encrusted with a
growth of bryozoa so that it is possibly a shell derived from an
older fossiliferous series.”

The presence of C. henekeni amandusi in the lower Miocene of
Lower California indicates that a western movement was made
before the land bridge between North and South America was
formed.

It seems likely, since the “C. henekeni group” was so well
established in Miocene time, that some Eocene ancestor will
possibly be found when collecting becomes more extensive in the
Caribbean Region. This statement, of course, is based on present-
day knowledge of fossil forms.

Today, C. isabella has a wide Indo-Pacific distribution, having
been reported by Ingram 1937a, 1937b, 1938, 1939a, 1939b, from
the Hawaiian Islands, Christmas, Washington, Palmyra, and Fan-
ning Islands, Guam Island in the Mariana Group, American
Samoa, and Makatea Island in the Tuamoto Archipelago, and
from numerous localities by Schilder and Schilder (1939). C.
isabella Linnzeus has survived as a plastic species from Miocene
time, and is one of the most common cowries in number of indi-
viduals throughout its present distributional range. It has been re-
ported from the middle Miocene of Santo Domingo by Pilsbry
(1921), Gabb (1873), Maury (1917), and Ingram (1939e).
Woodring (1928) listed a subspecies, Cyprea isabella patrespa-
trie Maury, from the Bowden fauna of Jamaica (middle Mio-
cene). Pilsbry (1921) and Ingram (1939e) consider Maury’s
patrespatrie to be a synonym of the species C. isabella. The dis-
tribution of the subspecies C. isabella mexicana Stearns, the ap-
parent local descendant of the Miocene isabella, has been recorded
vy Hertlein (1937). This worker listed the following localities
where the subspecies is known to occur: Tres Marias and
Revillagigedo Islands; Gulf of California; Cape San Lucas,
Lower California; and Clipperton Island. Specimens listed as
types are numbered 46581 in the United States Natsonal Museum

101 CyPr4ID& or NortH AMERICA: INGRAM 11

and are from Tres Marias, Gulf of California. The Miocene col-
lection from. Santo Domingo is the oldest collection geologically
and older than any fossil collections of isabella from the Indo-
Pacific region. From present data, it seems likely that the living
Indo-Pacific isabella originated in Miocene time in the Carib-
bean region. It then migrated eastward before the Canal Zone
formed a barrier.
NONEXISTENT FORMS

The author believes as have others working with the Cypreide,
notably Dall (1890), that the following species should be
placed in a doubtful group. The doubtful or nonexistent spe-
cies are Cyprea annulifera Conrad, Cyprea lapidosa Conrad,
Cyprea semen Tuomey, and Cyprea hemispherica Tuomey.

Dall (1890) stated that C. annulifera was merely a C. annulus
Linneus some Indian or trader may have dropped on _ the
Yorktown Peninsula. The writer has examined this specimen
in the Academy of Natural Sciences, Philadelphia, and also
determined it to be, without doubt, C. annulus Linnzeus. This
species is a typical Indo-Pacific form, being one of the most
common of Recent Cypreide. Concerning the remainder of the
above species it is well to cite Dall (1890) : “In Tuomey’s Report
on the Geology of South Carolina, 1848, among the Eocene fossils
enumerated are Cyprea lapidosa Conrad, C. semen and C. hemi-
spherica Tuomey. These are mere names, never having been
described or figured. The type of C. lapidosa is still to be found
in the museum of the Academy of Natural Sciences. It is an
unrecognizable internal cast which may not even be a Cyprea,”
The type of C. Japidosa in the above institution was examined by
the writer, and is obviously an unrecognizable internal cast, doubt-
fully that of a Cyprea.

A'ICKNOWLEDGMENTS

Grateful acknowledgment is made to the following individuals
who have aided in the preparation of this work, and to the fol-
lowing institutions which have courteously offered their material
for study: Prof. G. D. Harris and Dr. K. V. Palmer of the Pal-
eontological Research Institution, Ithaca, New York; Dr. C. W.

12 BuLuetin 104 : 102

Merriam of the Department of Geology of Cornell University,
Ithaca, New York; Dr. Paul Bartsch, Dr. Harald Rehder, and
Mr. F. S. MacNeil of the United States National Museum,
Washington, D. C.; Dr. Henry A. Pilsbry, Dr. B. F. Howell,
and Miss Anne Harbison of the Academy of Natural Sciences,
Philadelphia, Pennsylvania; Dr. C. Weaver of the Department
of Geology of the University of Washington, Seattle, Washing-
ton; Dr. G. Dallas Hanna and Dr. L. G. Hertlein of the Califor-
nia Academy of Sciences, San Francisco, California; Dr. Bruce
L. Clark of the Department of Paleontology of the University of
California, Berkeley, California; Dr. Charles T. Berry of the
Johns Hopkins University, Baltimore, Maryland, and Mr. Will-
iam T. Clark, Jr., of Cambridge, Massachusetts.

The United States National Museum, Washington, D. C.; the
Academy of Natural Sciences, Philadelphia, Pennsylvania;
Paleontological Research Institution, Ithaca, New York; Cali-
fornia Academy of Sciences, San Francisco, California; the
Wagner Free Institute of Science, Philadelphia, Pennsylvania;
and the Geology Department of Cornell University, Ithaca, have
extended every privilege to aid in the preparation of this paper.

Gratitude is expressed to Dr. W. E. Heming of Whittier Col-
lege, Whittier, California, formerly of Cornell University, for
checking the numerous early drafts.

Sf OF EY PE-HOSSiL (GY PRASIDAD, OF
NORTH AMERICA

Genus CYPRBA Linneus, 1758

Cyprea alabamensis de Gregorio3
C. alabamensis de Gregorio, 1890, Annales de Géologie et de Paléontologie
Pp. 99; pl. 9, figs, 8-110)
Holotype.—DeGregorio home, Via Mola 132, Palermo, Sieily.
Type locality.—Gosport sand, Claiborne, Alabama. Middle Eocene.
Cyprza ballista Dall Plate ol, fiesesless
C. ballista Dall, 1915, United States National Museum Bulletin, 90 D
So; pluG: figs: 9.10 ate Gab
Holotype.—Numbered 165098 in United States National Museum.
Type locality.—Tampa silex beds at Ballast Point, Tampa Bay, Florida
8’ The specific description references are not repeated in the bibliog-
raphy unless they are cited in discussions in the text. aa

103 Cypraipa or NortH AMERICA: INGRAM 13

Cyprea bayerquei Gabb
C. bayerquei Gabb, 1864, Geological Survey of California, Paleontology,
vol. 1, pp. 129-130. Not C. bayerquei Gabb, 1869, Geological Survey
of California, Paleontology, vol. 2, pp. 163-164, pl. 27, figs. 43a, 43b,
43¢e.

Holotype—Numbered originally 31403 in the Museum o# Paleontology,
University of California, Berkeley, California; reported missing by Dr.
Bruce L. Clark of the Department of Paleontology.

Type locality.—Clayton, Contra Costa County, California. Upper Eocene,
Cyprea carolinensis Conrad

C. carolinensis Conrad, 1841, Silliman’s Journal, vol. 41, p. 346, pl. 2,

fig. 6.

Holotype.—?

Type locality—Natural Well, Duplin County, North Carolina. Upper
Miocene.

Cyprza carolinensis floridanus Mansfield Plate 1, figs. 3, 4

C. carolinensis floridanus Mansfield, 1931, Proceedings of the United

States National Museum, vol. 79, p. 6, pl. 1, figs. 2, 6, 7.

Holotype.—Numbered 371333 in the United States National Museum.

Type locality—Tamiami Trail, 42 miles west of Miami, Florida. Upper
Miocene.

Cyprza castacensis Stewart Plate 1, figs. 5, 6

C. bayerquei Gabb, 1869, Geological Survey of California, Paleontology,

vol. 2, pp. 163-164, pl. 27, figs. 43a, 43b, 48¢e.

C. castacensis Stewart, 1926, Proceedings of the Academy of Natural

Sciences, Philadelphia, vol. LX XVIII, p. 370, pl. 28, fig. 10.

Holotype—Numbered 11690 in the Museum of Paleontology, University
of California, Berkeley, California. Reported missing by Dr. Bruee L.
Clark of the Department of Paleontology.

Type locality.—University of California locality 452, Grapevine Creek,
Tejon, California. Upper Eocene.

Cyprea chilona Dall Plate 1, figs. 7, 8

C. chilona Dall, 1900, Transactions of the Wagner Free Institute of

Science, vol. 3, pt. 5, p: 1195, pl. 39). figs. 1, 3.

Lectotype-—Numbered 498388 in the United States National Museum,
Washington, D. C.

Type locality.—Chipola beds, Alum Bluff, Florida. Middle Miocene.
Cyprza eosmithii Aldrich

C. smithii Aldrich, 1886, Geological Survey of Alabama, Bulletin 1, p.

Siay, Jol, 1), tees Bh
C. eosmithii Aldrich, 1923, Proceedings of the Biological Society of
Washington, vol. 36, p. 199.

Holotype.—Aldrich collection, not numbered. The Johns Hopkins Uni-
versity, Baltimore, Maryland.

Type locality.—Gregg’s Landing, Alabama. Sabine, Eocene.

Cyprza estellensis Aldrich ;

C. estellensis Aldrich, 1921, Bulletin of American Paleontology, vol. 9,

No. 37, pp. 14-15, pl. 2, fig. 1.

Holotype——Alabama State Museum.

Type locality.—Suearnoochee beds, Pursley Creek, Wilcox County, Ala-
bama. Sabine (Wilcox) Eocene.

Cyprea fresnoénsis Anderson Plate 1, fig. 9

C. fresnoénsis Anderson, 1905, Proceedings of the California Academy of

Sciences, third series, vol. 2, No. 2, p. 198, pl. 13, fig. 2.

14 BULLETIN 104 104

Holotype.—Numbered 50, California Academy of Sciences, San Fran-
cisco, California.

Type locality—Avenal sands, northwest of Coalinga, western Fresno
County, California. :

Cyprea healeyi Aldrich Plater 2 fig sali 2a ome

C. healeyi Aldrich, 1923, Proceedings of the Biological Society of Wash-

ington, vol. 36, p. 199.

C. dalli Aldrich, 1894, The Nautilus, vol. 7, No. 9, p. 98, pl. 4, figs. 2, 2a.

Holotype-—Numbered 135157 in the United States National Museum.

‘Type locality—United States National Museum number 319, Red Bluff,
Chickasawhay railroad bridge, one and one-half miles south of Shubuta,
Clark County, Mississippi. Oligocene.

Cyprea heilprini Dall Plate 2, figs. 5, 6

C. heilprinii Dall, 1890, Transactions of the Wagner Free Institute of

Science, vol. 3, p. 166, pl. 11, figs. 2, 2a.

Holotype.—Numbered 114103 in the United States National Museum.

Type locality—Ballast Point, Chipola beds, Florida. Lower Miocene.
Cyprea henikeni amandusi Hertlein and Jordan

C. amandusi Hertlein and Jordan, 1927, Proceedings of the California

Academy of Sciences, fourth series, vol. 16, pp. 628-629, pl. 18, fig. 1,
jolle Gy savers, al, 2h, Bi

Types.-Syntypes in Leland Stanford University type collection from
locality 66 of Stanford University, California. Paratypes numbered 2663
and 2664 in the California Academy of Sciences, San Francisco, California.

Type locality-—San Ignacio Arroyo, 8 kilometers southwest of San Ig-
nacio, Lower California. Insidro formation. Lower Miocene.

Cyprza jacksonensis Johnson Plater 2 eaten
C. jacksonensis Johnson, 1899, Proceedings of the Academy of Natural
Sciences, Philadelphia, vol. 5, p. 77.

Holotype.—Numbered 7120 in the Academy of Natural Sciences, Phila-
delphia.

Type locality-—Jackson, Mississippi. Upper Eocene.

Cyprea kempere Nelson Plate 2, figs. 8, 9

C. kempere Nelson, 1925, University of California Publications in Geo-

logical Sciences, vol. 15, p. 424, pl. 56, figs. 9, 10; pl. 57, fig. 4.

Holotype.—Numbered 987 in the California Academy of Sciences San
Francisco, California; Syntype, numbered 30541 in the Museum of Paleon-
tology, University of California, Berkeley, California.

Type locality.—University of California locality number 3764 in the
Martinez south of Simi Valley, Ventura County, California. Martinez
Kocene. Lower Eocene.

Cyprza kennedyi Harris

C. kennedyi Harris, 1895, Proceedings of the Academy of Natural Sei-

ences, Philadelphia, vol. 47, p. 78, pl. 8, figs. 12, 12a.

Holotype.—Texas State Museum (Harris 1895). Formerly in the Geol-
ogy Department, University of Texas, Austin, Texas. Probably lost, Palmer
(1937).

Type locality.x—Dr. Collard’s farm, Town Branch, Sparks Headright,
Brazos County, Texas. Lower Claiborne Eocene,

105 Oypraips® oF NortH AMERICA: INGRAM 15

Cyprza ludoviciana Johnson Plate 2, figs. 10, 11
C. ludoviciana Johnson, 1899, Proceedings of the Academy of Natural
Sciences, Philadelphia, vol. 51, pp. 77-78, pl. 2, fig. 6.
Lectotype-—Numbered 13538 in the Academy of Natural Sciences, Phila-
delphia.
Type localityx—Montgomery, Grant Parish, Louisiana. Jackson Eocene.
Upper Hocene.
Cyprea mathewsonii Gabb Plate 2, fig. 12
C. mathewsonii Gabb, 1869, Geological Survey of California, Paleontol-
ogy, vol. 2, p. 164, pl. 27, figs. 44a, 44b.
C. kerniana Anderson and Hanna, 1925, Occasional Papers of the Cali-
fornia Academy of Sciences, vol. 11, pp. 104-105, pl. 13, figs. 9, 10, 11.
Holotype.—Numbered 4217 in the Academy of Natural Sciences, Phila-
delphia, Pennsylvania.
Type locality—Tejon group, Martinez, California. Upper Hocene.
Cyprza novasumma (Nelson) Plate 2, fig. 13
Ovula novasumma Nelson 1925, University of California Publications
in Geological Sciences, vol. 15, No. 11, p. 425, pl. 57, fig. 2.
Holotype—Numbered 30499 in the Museum of Paleontology, University
of California, Berkeley, California.
Type locality.—Martinez, south side of Simi Valley. Martinez Hocene.
Lower Eocene.

Cyprza nuculoides Aldrich Plate 2, fig. 19
C. nuculoides Aldrich, 1903, The Nautilus, vol. 16, No. 9, p. 98, pl. 3,
figs. 4, 5, 6.

Holotype.—Geology Department of the Johns Hopkins University, Bal-
timore, Maryland. Specimens in the Aldrich collection are not numbered.

Type locality—Dubose’s Mill in west Alabama. Claiborne, middle Eo-
cene.

Cyprea oakvillensis Van Winkle Plate 2, figs. 14, 15

C. oakvillensis Van Winkle, 1918, University of Washington Publications

in Geology, vol. 1, No. 2, p. 88, pl. 7, fig. 19.

Holotype-—Numbered 7606 in the California Academy of Sciences, San
Francisco, California.

Type locality.—University of Washington Paleontological locality num-
ber 161, about one mile west of Oakville on the Northern Pacifie Railway.
Lower Oligocene; Barbatia merriami zone.

Cyprea pilsbryi Ingram Blater 2) fics: 165017,

C. pilsbryi Ingram, 1939, The Nautilus, vol. 52, No. 4, pp. 120-121, pl.

9, figs. 2a, 2b.

Holotype.—Numbered 781 in the Aeademy of Natural Sciences, Phila-
delphia, Pennsylvania.

Type locality.—Along the Cape Fear River, North Carolina. Miocene.
Cyprza pinguis Conrad

C. pinguis Conrad, 1854, in Wailes Report on the Agriculture and Geolo-

gy of Mississippi, pl. 17 (corrected plate number) ; reprint 1939, Bul-
letin of American Paleontology, vol. 24, No. 86, p. 8, pl. 17, figs. 3a, 3b.

Holotype.—?

Type locality—Jackson, Mississippi. Upper Eocene.

Cyprza simiensis Nelson Plate 2, fig. 18
Lo: simiensis Nelson, 1925, University of California Publications in Geolo-

16 BULLETIN 104 106

gical Sciences, vol. 15, p. 425, pl. 57, figs. 3a, 3b, 3e.

Holotype.—Numbered 30498 in the Museum of Paleontology, University
of Calitornia, Berkeley, California.

Type locality.—Loeality number 3818 of the Museum of Paleontology of
the University of California. Martinez Eocene.

Cyprza sphzroides Conrad Plate 3) figstelees

U. sphaeroides Conrad, 1847, Proceedings of the Academy of Natural

Sciences, Philadelphia, vol. 3, p. 282.

Lectotype.—Numbered 13512 in the Academy of Natural Ssiences, Phila-
delphia, Pennsylvania.

Type locality.—Vicksburg, Mississippi. Oligocene.

Cypreza squyerii Campbell Plate 3, figs. 3, 4

C. squyerti Campbell, 1892, The Nautilus, vol. 6, No. 5, pp. 50-51. (Named

but not deseribed.)

C. squyerii Campbell, 1893, The Nautilus, vol. 7, No. 5, p. 52, pl. 2, figs.

1, 2. (Described and figured.)

Holotype.—Numbered 13536 in the Academy of Natural Sciences Phila-
delphia, Pennsylvania.

Type locality—Mingusville, Montana. Cretaceous.

Cyprza suciensis Whiteaves
C. suciensis Whiteaves, 1895, Proceedings and Transactions of the Royal
Society of Canada, second series, vol. 1, section 4, No. 4, pp. 119-134,

Holotype.—In the Museum of the Geological Survey ef Canada.

‘Type locality.—Sucia Islands, Vancouver, British Columbia. Cretaceous.
Cyprza tumulus Heilprin Plate 3, fig. 5

C. tumulus Heilprin, 1887, Transactions of the Wagner Free Institute of

Science, vol. 1, p. 111, pl. 16, figs. 49, 49a.

Holotype.—Numbered 861 in the Wagner Free Institute of Science, Phil-
adelphia, Pennsylvania.

Type locality—Ballast Point, Hillsboro Bay, Florida. Lower Miocene.
Cyprza vaughani Johnson Plate 3, figs. 6, 7

C. vaughani Johnson, 1899, Proceedings of the Academy of Natural

Sciences, Philadelphia, vol. 51, p. 78, pl. 2, fig. 7.

Holotype.—Numbered 9450 in the Academy of Natural Sciences, Phila-
delphia, Pennsylvania.

Type locality—Hammett’s Branch near Mt. Lebanon, Louisiana. Lower
Claiborne Eocene.

Cyprza willcoxi Dall Plate 3, figs. 8, 9

C. willcoxi Dall, 1890, Transactions of the Wagner Free Institute of

Science, vol. 3, pp. 166-167, pl. 11, figs. 2, 2a.

Holotype.—Numbered 112441 in the United States National Museum,
Washington, D. C.

Type locality.—Two localities were cited by Dall (1890) in his deserip-
tion of this species; in the Chipola red sand, West Florida and at White
Beach, near Osprey, Florida, at the northern part of Little Sarasota Bay,
in a water-worn sandstone of yellowish-brown color, The holotype is from
White Beach, near Osprey, Florida. Middle Miocene.

107 Cyrraipz or Norton America: INGRAM Wy

CYERaan “OCCURING IN BOTH THE FOSSIL “AND
LIVINGSTATE IN NORTH AMERICA

Cyprea arabicula Lamarck
C. arabicula Lamarek, 1819, Suite du Genre Poreelaine, Annales Museum
National d’Histoire Naturelle, Paris, vol. 16, p. 100.

This species occurs in the Pleistocene of Magdalena Bay, Lower Cali-
fornia, (Jordan, 1986), and in the Pleistocene of Oaxaea, Mexico (Palmer
and Hertlein, 1936), (Grant and Gale, 1931).

Cyprea sowerbyi Kiener
C. sowerbyi Kiener, 1845, Species General Iconographie Coquilles, Cy-
prea, pp. 38-39, pl. 7, fig. 5.

C. annette Dall, 1909, The Nautilus, vol. 22, p. 125.

This species occurs in the Pleistocene of Magdalena Bay, Lower Cali-
fornia (Grant and Gale, 1931), (Jordan, 1936).

Cyprza spadicea Swainson
C. spadicea Swainson, 1823, Philosophical Magazine, vol. LXI, p. 376.
C. spadicea Gray, 1824, Monograph, Cypreide, Zoological Journal, vol. 1,
pp. 900-501.

C. fernandoensis Arnold, 1907, Proceedings of the United States Na-

tional Museum, vol. 32, p. 538, pl. 1, figs. 8, 8a.

This species has been reported from the Pleistocene and Pliocene of
California, (Arnold, 1907), (Gabb, 1869), (Grant and Gale, 1931), (In-
gram, 1938a) and from the Pleistocene of Magdalena Bay, Lower Califor-
nia, (Jordan, 1936).

K ok OK
Genus SIPHOCYPR/MA Heilprin, 1887

Heilprin (1887) proposed the name Siphocyprea as a sub-
genus. Here this name is given full generic rank. In establish-
ing Siphocyprea Heilprin stated, “I propose this subgenus for a
group of remarkable Cypreas, which differ from all other mem-
bers of the family in the possession of a deep, comma-shaped sul-
cus or depression, occupying the apical portion of the shell, and
which, as the poster?or continuation of the aperture, is curved
dextrally around the axis of involution ... The other characters
of the shell are those of the Cypreea generally.” (Heilprin, 1887.)
At this time the genotype is the only species included in the genus.

18 BULLETIN 104 108

Siphocyprza problematica Heilprin Plate 3, figs. 104 11

C. (S.) problematica Heilprin, 1887, Transactions of the Wagner Free

Institute of Science, vol. ly p. 87, pl. 4, figs. 12a; Web:

Lectotype.—Numbered 915 in the Wagner Free Institute of Science. By
personal communication, Mr. John G. Hope, Curator of the Wagner Free
Institute of Science, Philadelphia, states by letter, ‘‘ . . there are three
specimens in a tray from Caloosahatchie, Florida. These are marked
‘“types,’’ and agree with the three specimens figured by Heilprvin in ‘‘ Ex-
plorations in Florida, Transactions of the Wagner Free Institute of Science,
Vol. 1.’’ From these three specimens one should be selected as the lecto-
type; since the other two specimens were figured by Heilprin in the original
description they would no doubt be designated as paratypes.

Type locality.—Caloosahatchie formation, below Fort Thompson, Florida.
Pliocene.

Genus SULCOCYPR/KA Conrad, 1865

Conrad (1865) proposed the name Sulcocyprea as a subgenus.
Here this name is given full generic rank.

Sulcocyprza lintea (Conrad) Platense tie seealcamelts

C. lintea Conrad, 1847, Proceedings of the Academy of Natural Scei-

ences, Philadelphia, vol. 3, p. 282.

Lectotype-—Numbered 13510 in the Academy of Natural Sciences, Phil-
adelphia, Pennsylvania.

Type locality.—Vicksburg, Mississippi, Oligocene.

Conrad’s (1847) description is included here since it appar-
ently contained several errors which Aldrich (1894) corrected.
Aldrich’s (1894) corrections are also included.

Conrad’s (1847) original description states, “Ovate, elevated,
ventricose, with four approximate equal impressed lines; base
ventricose, profoundly striated; labrum margin much thickened,
profoundly striated; summit of labrum prominent; base slightly
produced.” Aldrich (1894) referring to the above description
states, “Conrad’s original description contains a misprint which
seems to have been perpetuated in later publications. It should
read “with fine approximate equal impressed lines,’ instead of
“four .. lines.” This writer examined the holotype and there is
no doubt but that Conrad’s original description should have read
fine instead of four.

Genus CYPRZAEDIA Swainson, 1840

Swainson (1840) in describing this genus stated, “Cypreform ;
the base contracted; the body-whorl not flattened beneath; shell

4 Figure 10 is here designated as the lectotype.

109 CyPpra&ipza or NortH AMERICA: INGRAM 19

cancellated; aperture of equal breadth throughout; a few thick-
ened, short teeth on the pillar; lip at the base which 1s not intern-
ally concave.” Three North American species belong to this genus.
These are C. gilberti Palmer, C. fenestralis Conrad, and C.
subcancellata (Johnson).

Cypredia fenestralis Conrad Plate 4, figs. 2, 3
C. fenestralis Conrad, 1854, in Wailes’ Report on the Agriculture and
Geology of Mississippi, pl. 17 (corrected plate number), figs. 3a, 3b, 3¢;
reprint, 1939, Bulletin American Paleontology, vol. 24, No. 86, p. 8,
pl. 4, figs. 5a, 5b.
Lectotype.-—Numbered 13197 im the Academy of Natural Sciences, Phila-
delphia, Pennsylvania.
Type locality—Jackson, Mississippi. Upper Eocene.
Cypredia gilberti Palmer Plate 4, figs. 4, 5
C. gilberti Palmer, 1937, Bulletin of American Paleontology, vol. 7, pts.
1, 2, pp. 234-235, pl. 30, figs. 27, 28.
Holotype——Numbered 2962 in the Paleontological Research Institution,
Ithaca, New York.
Type locality—Gosport sand, Monroe County, Alabama; Paleontological
Research Institution, No. 104. Claibornian, middle Eocene.
Cypredia subcancellata (Johnson) Plater4a fies!
C. subcancellata Johnson, 1899, Proceedings of the Academy of Natur-
al Sciences, Philadelphia, vol. 51, pp. 78- 79, pl. 2, fig. 9.
Holotype-—Numbered 7119 in the Academy of Natural Sciences, Phila-
delphia, Pennsylvania.
Type locality—Smithville, Bastrop County, Texas. Lower Claiborne
Eocene.

Genus GISORTIA Jousseaume, 1884

Coquille ovoide, déprimée en dessous, irréguliérement arrondie et souvent
tuberculeuse en dessus. Ligne d’ intersection du manteau centrale; ouver-
ture sinueuse dilatée en avant; bords peu ou point dentés, fossette antérieure
du bord columellaire a peine sensible.
Gisortia clarki Ingram Plate 4, fig. 1

G. clarki Ingram, 1940, Journal of the Washington Academy of Sciences,

vol. 30, No. 9, pp. 376-377, fig. 1.

Holotype.—Numbered 14844 in the Museum of Paleontology, University
of California, Berkeley, California.

Type locality.—Loeality number 4052, Museum of Paleontology, Univer-
sity of California; Capay stage, Llajas formation, lower zone, Simi Valley,
Ventura County, California. Eocene.

DOUBTEUL CYPRAIDAY

Two species of Cypreidz, both of the genus Cyprea, are con-
sidered to be of doubtful specific rank. These are Cyprea sabulov-
widis Whitfield, and Cyprea mortoni Gabb. Cyprea mortoni
Gabb is of extremely doubtful rank. The writer has examined
the holotype in the Academy of Natural Sciences, Philadelphia,
and found that its generic character was questionable. This spe-

20 BULLETIN 104 110

cies probably belongs to the Cyprzeidze, but since some of the can-
cellated genera of the family have a smooth interior, and would
leave a smooth internal mold like a member of the genus Cyprea,
it seems best to question the generic as well as the specific rank
of this species until a topotype showing shell characteristics 1s
found. No shell characters are preserved in the holotype. Only
the holotype illustrations of Cyprea sabuloviridis Whitfield have
been available to the writer; these show beyond doubt that this
species was based on an internal mold, thus one can question the
generic rank until topotype material is available. The illustra-
tions indicate that this species may belong to the Cypreeide,

Cyprza mortoni Gabb
C. mortoni Gabb, 1860, Journal of the Academy of Natural Sciences,
Philadelphia, second series, vol. 4, p. 391, pl. 68, fig. 8 in text, 9 in
plate.
Holotype-—Numbered 13535 in the Academy of Natural Sciences, Phila-
delphia, Pennsylvania.
Type locality Burlington County, New Jersey. Cretaceous.
Cyprza sabuloviridis Whitfield
C. sabuloviridis Whitfield, 1892, Monograph of the United States Geo-
logical Survey, vol. 18, p. 223, pl. 33, figs. 20, 21, 22.
C. sabuloviridis Whitfield, 1892, Geological Survey of New Jersey, vol.
2, pp. 1-402.
Holotype.—Rutgers University, New Brunswick, New Jersey.
Type locality ‘In the Upper layers of the Upper Green Marls at
Shark River, and Farmingdale, New Jersey.’’ (Whitfield, 1892.) Hocene.

Whitfield (1892) 1n both of the above references described this
species as new. The above cited reports are word for word pub-
lications. Since two separate localities are cited it is question-
able which should be chosen as the type locality.

alae Cypraipz or NortH AmeEricA: INGRAM 21

BIBLIOGRAPHY

Aldrich, T. H.
New Tertiary fossils from Red Bluff, Mississippi, The Nau-
tilus, vol. 7, No. 9, 1894, p. 98, pl. 4, figs. 2, 2a.
New species of Tertiary fossils from Alabama, Mississippi, and
Florida, The Nautilus, vol. 16, No. 9, 1903, p. 98, pl. 3, figs. 4,
5, 6.

Arnold, R.
New and characteristic species of fossil mollusks from the oil-
bearing Tertiary forma ion of southern California, Proe. U.
S. Nat. Mus. vol. 32, 1907, pp. 525-546.

Conrad, T. A.
Observations on the Locene formation, and descriptions of one
hundred and five new jossils of that period, from the vicinity
of Vicksburg, Mississippi, with an appendix, Proc. Acad. Nat.
Scei., Philadelphia, vol. 3, No. 11, 1847, pp. 280-299.
Calalogue o, the Loc-ne and Oligocene testacea of the United
States, Amer. Journ. Conch., vol. 1, 1865, p. 31.

Clark, B. L., and Vokes, H..E.
Summary of marine Locene sequence of western North Amer-
ica, Bull. Geol. Soc. Amer., vol. 47, 1936, pp. 851-878.

Dall, W. H.
Contributions to the Vertiary fauna of Florida, with especial
reference to the Miocene silea-beds of Tampa and the Pliocene
beds of the Caloosahaichie River, Trans. Wag. Free Inst. Sei.,
vol. 3, pt. 1, 1890, pp. 1-200.

Gabb, W. M.
On the topography a.d geology of Santo Domingo, Trans.
Amer. Phil. Soe., vol. 15, new series (read 1872), 1873, pp.
49-259.

Cretaceous and Tertiary fossils, Geol. Surv. of Calif., Paleon-
tology, vol. 2, 1869, pp. 1-299.

Grant, U. S., and Gale, H. R.
Pliocene and Pleistocene Mollusca of California and adjacent
regions, Memoirs of San Diego Soc. Nat. Hist., Calif., vol. 1,
1931, pp. 1-1036.

Harris, G. D.
Tertiary paleontology of Texas, Proce. Acad. Nat. Sei., Phila-
delphia, vol. 47, 1895, pp. 45-88.

Heilprin, A.
Explorations of the West Coast of Florida in the Okcechobee
Wilderness, Trans. Wag. Free Inst. Sci., vol. 1, 1887, pp. 1-134.

Hertlein, L. G.
A note on some species of marine mollusks oceuring in both
Polynesia and the western Americas, Proc. Amer. Phil. Soe.,
vol. 78, No. 2, 1937, pp. 303-312.

Ingram, W. M.
The family Cypreide in the Hawaiian Islands, The Nautilus,
vol. 50, No. 3, 1937 (a), pp. 77-88.
Cypreide from Christmas, Palmyra, Washington, and Fanning
Islands, The Nautilus, vol. 51, No. 1, 1937 (b), pp. 5-7.

19
92 BULLETIN 104 ny

—_____—. Cypreide from Guam, Tre Nautilus, vol. 52, No. 1, 1938, pp.

—_—_—— ie on the cowry, Cyprea spadicea Swainson, The Nautilus,
vol. 52, No. 1, 1938 (a), pp. 1-4.
Cypreide from American Samoa with notes on species from
Palmyra Island, The Nautilus, vol. 52, No. 3, 1939 (a), pp
103-105. :

______ Cypreide from Makatea Island, Tuamotu Archipelago, Oceas.
Papers, Bernice. P. Bishop Museum, vol. 14, No. 18, 1939 (b),
pp. 323-325.

______ Notes on Cyprea heilprini Dall and Cyprea chilona Dall with
new species from the Pliocene of Costa Rica, Bull. Amer. Pal-
contology, vol. 24, No. 84, 1939 (ce), pp. 321-326.

—_______ Endemic Hawaiian cowries, Oceas. Papers, Bernice P. Bishop
Museum, 14, No. 19, 1939 (d). pp. 327-333.
New fossil Cypreide from the Miocene of the Dominican
Republic and Panama, with a survey of the Miocene specics
of the Dominican Republic, Bull. Amer. Paleontology, vol. 24,
No. 85, 1939 (e), pp. 329-340.

Jordan, E. K., and Hertlein, L. G.
The Pleistocene fauna of Magdalena Bay, Lower California,
Cont. Dept. Geol. Stanford University, vol. 1, No. 4, 1936, pp.
107-173.

Jousseaume, F.
Etude sur la familie des Cypreide, Bull. Soe. Zool. Franee, t.
9, 1884, pp. 88-89.

Linnzus, C.

Systema Nature, Tomus 1, 1758.
Mansfield, W. C.

Miocene gastropods and scaphopods from Trinidad, British
West Indies, Proc. U. S. Nat. Mus., vol. 66, No. 2559, 1925,
pp. 1-65.

Maury, C. J.

Santo Domingo type sections and fossils, Bull. Amer. Paleon-
tology, vol. 5, No. 29, pt. 1 1917, pp. 1-252.

———— A further contribution to the Paleontology of Trinidad (Mio-
cene horizons), Bull. Amer. Paleontology, vol. 10, No. 42,
pp. 1-410.

Olsson, A. A.

Contributions to the Tertiary paleontology of Northern Peru,
Part 4, The Peruvian Oligocene, Bull. Amer. Paleontology, vol.
17, No. 63, 1931, pp. 1-264.

Ostergaard, J. M.

Fossil marine mollusks of Oahu, Bull. Bernice P. Bishop Mu-
seum, No. 51, 1928, pp. 1-32.

Palmer, R. H., and Hertlein, L. G.
Marine Pleistocene mollusks from Oaxaca, Mexico, Bull. 8.
Cal. Acad. Sci., vol. 35, pt. 2, 1936, pp. 65 to 81.

Palmer, K.

The Claibornian Scaphopoda, Gastropoda, and dibranchiate

Cephalopoda of the southern United States, Bull. Amer. Pal-
eontology, vol. 7, No. 32, 1937, pp. 230-237.

113 Cypraip& or NortH AMERICA: INGRAM 23

Pilsbry, H. A.
Revision of W. M. Gabb’s Tertiary Mollusca of Santo Do-
mingo, Proce. Acad. Nat. Sei., Philadelphia, vol. 73, 1921, pp.
305-435.

Pilsbry, H. A., and Olsson, A. A.
The Pliocene fauna from western Ecuador, Proce. Acad. Nat.
Sei., Philadelphia, 1941, p. 41, pl. 7, fig. 4.

Schilder, F. A.

Additions and corrections to Vredenburg’s classification of the
Cypreide, Ree. Geol. Sur. India, vol. 58, pt. 4, 1926, pp. 358-
379.
Fossilium Catalogus, 1: Animalia, Pars 55: Cypra@acéa. Puab-
lished by W. Junk, Berlin, 1932.
Cypreacea aus dem Tertiar von Trinidad, Venezuela, und den
Antillen, Abh. der Schweiz. Paleont. Gesell., Bd. 62, 1939, pp.
1-35.

Schilder, F. A., and Schilder, M.
Prodrome of a monograph on living Cypreidxe, Proce. Mal.
Soc. London, vol. 23, pt. 4, 1939, pp. 119-231.

Sowerby, G. B.
Thesaurus Conchyliorum, Cyprea, pts. 26, 27, 28, 1870, pp.
1-58. London.

Stefano, G. di
Nuove spec. tithoniche, Natural. Siciliano, vol. 1, 1882.

Stearns, F. E. C.
On rare or little known mollusks from the West Coast of North
and South America, with descriptions of new specics, Proe.
U. S. Nat. Mus., vol. 16, No. 941, 1893, pp. 341-352.

Swainson, W.
A treatise on Malacology, In the Cabinet Cyclopedia, edited
by D. Lardner, 1823, p. 325.

Trechmann, C. T.
The yellow limestone of Jamaica and its mollusks, Geol. Mag.,
London, vol. 60, No. 8, 1923, pp. 337-367.

Tuomey, M., and Holmes, F. S.
Pliocene fossils of South Carolina, Russel and Jones, Publish-
ers. 1857.

Vredenburg, E.
Classification of the, Recent and fossil Cypreide, Rec. Geol.
Sur. India, vol. 2, pt. 1, 1920, pp. 65-152.

Whitfield, R. F.
Gasteropoda and Cephalopoda of the Raritan clays and Green-
sand marls of New Jersey, Geol. Surv. New Jersey, vol.
1892, pp. 1-402. ;
Gasteropoda and Cephalopoda of the Raritan clays and Green-
sand marls of New Jersey, Mon. U. 8. Geol. Survey, vol. 18,
1892, pp. 1-402.

Woodring, W. P.
Miocene mollusks from Bowden, Jamaica, Part two, Carnegie
Inst. Wash., Pub. No. 385, 1928, pp. 316-321.

€
=)

*

PLATES

PLATE 1 (8)

26 BULLETIN 104 116
EXPLANATION OF PLATE 1 (8)
Figure Page
1-2) Cypreauballistal Dall ie ee ee 12
Holotype; natural size.
3-4. Cyprea carolinensis floridanus Mansfield 13
Holotype; natural size
5-6. Cyprza castacensis Stewart —_ oe eee ath = A 13
Approximately natural size.
768. Gypreachilona Dall {2222.2 ee 13
Lectotype; natural size.
9. C€yprea fresnoéensis’ Anderson) 2-2 eee 13

Holotype; natural size

Buu. AMER. PALEONT. No. 104, Pu. 1

Pu. 8, VOL. 27

;

PEAT Ez, (©)

28
Figure
1-2. Cypreza healeyi Aldrich —_
Holotype; X38.
3-4, Cyprza healeyi Aldrich
Immature specimen; X2.
5-6. Cyprea heilprini Dall ——
Holotype; natural size.
7. Cyprza jacksonensis Johnson
Holotype; natural size.
8-9. Cyprea kemperz Nelson ___
Natural size.
10-11. Cyprza ludoviciana Johnson
Lectotype; X2.
12. Cyprea mathewsonii Gabb
Holotype; natural size.
13. Cyprea novasumma (Nelson) — ~
Holotype; natural size.
14-15. Cyprea cakvillensis VanWinkle
Holotype; natural size.
16-17. Cyprea pilsbryi Ingram PS Pu ey Pine
Holotype; natural size.
18. Cyprza simiensis Nelson —__
Holotype; natural size.
19. Cyprea nuculoides Aldrich

BULLETIN 104 118

EXPLANATION OF PLATE 2 (9)

Holotype; natural size.

Buu. AMER. PALEONT. No. 104, Pu. 2

Pu. 9, Vou. 27

30 BULLETIN 104 120

EXPLANATION OF PLATE 3 (10)

Figure Page

1-2. Cyprza shperoides Conrad wo By he ete ee 16
Lectotype; natural size.

3-4. Cyprzea squyeri Campbell — _.._.____. Ben 16
Holotype; X2.

ba (Cypreal tumulius) Heprine ee ee 16

Approximately natural size.

6-72 Cyprea vaurhani Johnson) EEE Eee 16
Holotype; X4.

8-9. Cyprza willcoxi Dall ies 16

Holotype; natural size.

10-11. Siphocyprza problematica Heilprin Seve a rr
Figure is the lectotype. Figure 11 is a paratype. Both na-
tural size.

12-13. Suleocyprwa lintea (Conrad)
Lectotype; X2.

Pu. 10, Vou. 27 Buu. AMER. PALEONT. No. 104, PL. 3

¥
Y

)
if 4
()
%
2,

PEATE 2 Gm)

32 BULLETIN 104 122

EXPLANATION OF PLATE 4 (11)

Figure Page
1. Gisortia clarki: Ingram (2-2 ee Eee 19
Holotype; natural size.
2-3) \Cypredia ftenestralis; Conrady) eee 19
Lectotype; natural size.
4-5. Cypredia gilberti Palmer AUS ee oe 19
Holotype. Figure 4, approximately X1.5; figure 5, X2.
6-75 Cypredia subeancellata) Gohnson)) eee 19

Holotype; X2.

Pu. 11, Vou. 27 Buu. AMER. PALEONT. No. 104, Pu. 4

etn a0
eh byl *
WRT (

~ BULLETIN

—

OF

iIg42

Paleontological Research Institution

Ithaca, New York

1

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 105

CEPHALOPODS FROM THE CLINTON GROUP
OF NEW YORK

By

7

Rousseau H. Flower
University of Cincinnati

AUOUSE 37, TOL2

Paleontological Research Institution
Ithaca, New York
Wie Se ae

ee

| Ya TD:
oe YOOI0OS S08 cy

AD
ee COMM BHUTHON AD

CONTENTS

HieieO Oi CRONe de en ANS UAL ere AE Anes. a

Cephalopods previously reported from the Clinton of New York
Description of species
Genus Armenoceras Foerste
A. subvertebratum Flower, n. sp.
Genus Leurocyecloceras Foerste
L. ringuebergi Flower, n. sp.
Genus Kionoceras Hyatt
KeSmilba bile s Hower ane spe teers Se eB
Genus Dawsonoceras Hyatt
D. americanum (Foord)

L. clintonense Flower, n. sp.
References
Plates

CEPHALOPODS FROM THE CLINTON GROUP OF
NEW YORK
By

RoussEAU H. FLOWER
University of Cincinnati

INTRODUCTION

The present study is largely concerned with the description of
cephalopods from the Irondequoit limestone of the Clinton group,
Middle Silurian, of western New York. This is based upon
material collected by Ringueberg and Sarle and now deposited
in the Buffalo Museum of Science. I wish to express my indebt-
edness to the Museum and to Dr. I. G. Reimann for an oppor-
tunity to study this interesting material.

Happily the cephalopods from the Clinton of New York de-
scribed by Hall have been restudied by Foerste in various papers,
and our knowledge of these forms is brought as near to comple-
tion as the scanty horizon data and the poor preservation of the
types permit. The twelve described species are briefly listed be-
low with the references to the more critical descriptions. One
of these species may be Lockport in age rather than Clinton; the
five described from the Rochester shale are known from flattened
material; several others are inadequately known, and the pre-
cise origin of several in terms of present-day stratigraphy is un-
certain. In view of the rather unsatisfactory condition of these
known forms, the few cephalopods here described from the Iron-
dequoit actually constitute a very considerable contribution to
the nautiloid fauna, containing nine determinable new species,
and the ubiquitous Dawsonoceras americanum. In addition, liv-
ing chambers of smooth orthoceracones indicate the presence of
at least two additional species which cannot be described until
the phragmocones have been found and studied.

6 BULLETIN 105 128

Faunally and systematically, the small group of cephalopods is
of more than usual interest. The problem of the correlation of
the Middle Silurian of New York with that of Indiana, Ohio, and
Illinois is still very complex. Outside of New York, there has
been no wide agreement as to the placing of the boundary be-
tween the Clinton and the Lockport. In New York, the lime-
stones and shales of the Clinton in general furnish a sharp litho-
logical contrast to the dolomites of the Lockport, but in the east-
central area there seems to be great lithological similarity between
the two divisions of the Middle Silurian. Further, no good
faunal criteria have yet been found to mark the two divisions
which can be regarded as infallible. It is probable that all pre-
Racine beds in the east-central area may be safely referred to the
Clinton. The present study offers some slight contribution to
the support of this belief in that it establishes the presence of some
supposedly characteristic Lockport genera in beds which are un-
cisputably Clinton in age. As a consequence, the presence of
such forms in pre-Racine strata in the east-central area cannot
be considered as indicating Lockport age, as was formerly sup-
posed.

CEPHALOPODS PREVIOUSLY REPORTED FROM EE
CLINTON OF NEW YORK

The previously described species of cephalopods of the Clinton
group of New York are few, and many of them are not adequate-
ly known at the present time. The largest number of species re-
ported are from the Reynales limestone.

Armenoceras vertebratum Hall (1852, p. 94, pl. 20, figs. 1a-g;
ee also Foerste, 1928, p. 220, pl. 41, figs. 1-6). Described from
the Reynales limestone of Reynales Basin, Niagara County, New
York:

Michelinoceras (?) virgulatum Hall (1852, p. 95, pl. 20, figs.
Za-c; see also. Foerste, 1928, pl. 45, fig. 5). This as reported
by Hall as occuring in association with the preceding, and also
at Lockport, New York, in the lower part of the Clinton. The
species is very inadequately known. Apparently conspecific
forms have been obtained from the [rondequoit limestone, but

129 CLINTON CEPHALOPODS: FLOWER 7

are thus far obtained only from silicified specimens inadequate
for the necessary study of the internal structure.

Oncoceras (2) subrectum Hall (1852, p. 94, pl. 28, fig. 11a, b).
This species is not adequately known for generic determination,
the type consisting of a rapidly expanding phragmocone of some
breviconic form. It is reported from the “lower silicious layers”
of the Clinton group at Lockport. Possibly this is to be attributed
to the Irondequoit rather than the Reynales limestone.

Discosorus conoideus Hall (1852, p. 99, pl. 28, figs. 13a-c).
According to Hall, the species is from the green shale near the
ridge road in the town of Ontario, Wayne County, and also in
the “lower part of the group” at Lockport, Niagara County,
New York. Foerste (1934, pp. 171-173) regards the horizon as
probably Reynales.

Leurocycloceras clavatum Hall (1852, p. 104, pl. 31, figs. 4a-b;
see also Foerste, 1928, p. 214, pl. 45, fig. 6). From the Herki-
mer sandstone, Herkimer County, New York. (Flower, 1941.)

Amphicyrtoceras (?) abruptum Hall (1852, p. 97, pl. 29, figs.
4a-b; see also Foerste, 1928, pp. 223-225, pl. 46, figs. 6a-b).
Enough is not known of this species to determine its exact generic
position. It might be referred to Ectocyrtoceras Foerste with
equal justification. The horizon of this species is uncertain.
Foerste’s statement concerning the occurrence of this form is as
follows: “This specimen was sent to Hall by Col. Jewett, of
Lockport, New York, as coming from the upper limestone in the
Clinton of that place, but for some unknown reason is referred
by Whitfield and Hovey to some part of the Clinton at Reynales
Basin. It is doubtfully listed by Chadwick from the Irondequoit,
but in a letter to the writer he recognizes the possibility of its
being Gasport age. If this species is properly placed in the
Clinton, which seems doubtful, it is the earliest occurrence of
depressed breviconic cyrtoceracones in pre-Lockport strata in
America.

Dawsonoceras americanum (Foord) is listed as occurring in
the Clinton in shales below the ore beds at Wolcott, Wayne
County, New York. The specimen figured by Hall (1852, p.
96, pl. 29, fig. 3) is rather poorly preserved and considerably flat-
tened, The surface markings, as represented here, lack the fes-
tooning characteristic of Dawsonoceras americanum or D. an-

8 BULLETIN 105 130

nulatwm. The location of this specimen does not seem to be
known. .

The Rochester shale carries a more abundant fauna than other
members of the Clinton, but the species are rather inadequately
known, owing largely to the poor state of preservation. The fol-
lowing are reported from the Rochester shale:

Dawsonoceras americanum (Foord). Though the original
Cescription was based upon several specimens from different lo-
ealities and horizons in the Silurian of America, the type, selected
by Foerste (1928, p. 35), is from the Rochester shale, and this
form is therefore the typical one.

Leurocycloceras rochesterense Foerste (1928, p. 224, pl. 53, fig.
1). This is Orthoceras imbricatum Hall, 1851, not Hisinger.

Kionoceras subcancellatum (Hall). Originally figured as
Orthoceras cancellatum. Known only from flattened portions of
the shell.

Kionoceras rochesterense Foerste (1928, p. 307). Originally
figured as Orthoceras virgatum? Sowerby (Hall, 1852, p. 291,
pl. 63, figs. 2-3).

Amphicyrtoceras subcancellatum (Hall) (Cyrtoceras ? can-
cellatum Hall, 1852, p. 290, pl. 61, figs. 2a-c). This is a flattened
brevicone of the general form of Amphicyrtoceras, but is known
only from flattened specimens. This supplies the only authentic
record of depressed breviconic cyrtoceracones in the Clinton of
New York. The reference of Amphicyrtoceras (?) abruptum
to the Irondequoit is highly questionable as noted above.

DESCRIPAION OF SPECIES

Genus ARMENOCERAS Foerste
Armenoceras subvertebratum Flower, n. sp. Plate 2, fig. 5

Conch orthoceraconic, depressed in section, expanding in the
type from 14 mm. and 16 mm. to 30 mm. and 20 mm. in a length
of 90 mm. The sutures are straight and probably slightly oblique,
being slightly inclined orad on the dorsal side. The camerz occur
six in a length equal to the adoral conchial width throughout the
known portion of the shell. The septa are deeply curved, having
% depth of 8 mm. at a conchial width of 25 mm., which is equal
to the depth of one and a half camer. The siphuncle is subcen-
tral in the early portion of the shell, but rapidly moves to a posi-

131 CLINTON CEPHALOPODS: FLOWER 9

tion well ventrad of the center, so that at a shell width of 30 mm.
the center of the siphuncle is located 4 mm. from the ventral wall.
The segments of the siphuncle are slightly expanded for Armeno-
ceras and are very similar to those of A. vertebratum (Hall) of
the underlying Reynales limestone. The recurved portion of the
neck is short, but at the adapical end of the segment a consider-
able area of adnation is developed. A typical segment at a conchial
width of 25 mm. has a length of 6 mm, and expands from 4 mm.
to 7mm. The camere continue to the adoral end of the specimen
without any trace of either the living chamber or any gerontic
features. Within the siphuncle annulosiphonate deposits are de-
veloped; adapically traces of horizontal radial canals typical of
the Sactoceratidze and some Armenoceras can be seen. Episeptal
and hyposeptal deposits are developed in the camerz and as usual
are markedly concentrated on the siphonal side of the shell.

Discussion.—This species agrees with Armenoceras vertebra-
tum (Hall) (see Foerste, 1928, p. 220, pl. 41, figs. 1-6) in general
aspect, particularly in the depth of the camere and the appearance
of the siphuncle, but differs from it in the depressed section and
the ventral position of the relatively small siphuncle in the mature
portion. Although the siphuncle in A. subvertebratum is appar-
ently subcentral in the earliest known stage, comparable stages of
A. vertebratum have not been figured. Quite probably such
stages alone would not be distinguishable.

A. subvertebratum is represented by two specimens, one of
which has furnished the basis of this description. The other spe-
cimen is unsuitable as a basis for determination due to its dis-
torted condition, but quite evidently it is conspecific with the
first.

Type.—Holotype, Buffalo Museum of Science, No. E1077.

Occurrence.—From the Irondequoit limestone, at Gasport,
New York.
Genus LEUROCYCLOCERAS Foerste

Leurocycloceras Foerste (1928, p. 272), based upon Leurocy-
cloceras raymondi of the Racine dolomite of Wisconsin, was
erected for the reception of annulated orthoceracones which dif-
fer from Cycloceras in lacking any fine transverse markings. The
genus has been revised by the writer (Flower, Amer. Jour. Sci.,
1941, vol. 239, No. 7) to include also forms which develop such

10 BULLETIN 105 132

broad flat annuli that the interspaces appear as narrow striz on an
otherwise smooth exterior. The genus contains most of the Sil-
urian species of America which have been referred to Cycloceras,
and also some which have been placed in Getsonoceras. The
essential diagnostic features of the genus are internal, and al-
though they are lacking in the species described below, which is
known only from a living chamber, this form is so similar to
several better known representatives of the genus that there is
no doubt concerning its relationship.

Leurocyeleceras ringuebergi Flower, n. sp. Plate 1, fig. 9

This species is known only from a living chamber, which is
130 mm. long, expanding from 28 mm. and 29 mm, to 35 mm.
and 36 mm. Expansion is more rapid over the basal than on the
adoral part, indicating the approach of maturity. The suture is
straight and transverse. The septum has a depth of 7 mm, at
a diameter of 28 mm. Half of the septum is preserved, but no
trace of the septal foramen remains.

Surface features in the form of shallow distant impressed bands
appear on the living chamber. Five to six bands occur in a length
cf 20 mm. As in other species, the bands are somewhat oblique.

Discussion.—The bands are much more closely spaced than
in L. buchert Flower (1941), and the rate of expansion is slight-
ly greater. Turther, that species attains a larger size while still
lacking any trace of mature features. The surface features are
also more closely spaced than in L. clavatum (Hall) of the Herk-
imer sandstone of the Clinton group of New York. The species
is much smaller than L. niagarense, and the surface markings are
more distant than in comparable portions of that form.

Type.—Buffalo Museum of Science, No. E10672

Occurrence.—Irondequoit limestone, Clinton group, Middle
Silurian, from Lockport, New York.

Genus KIGNOCERAS Hyatt
Kionoceras mutabile Flower, n. sp. Plate 1, figs. 1-4

This species, represented by several specimens from the Jron-
dequoit, is characterized by the change of ornament which ranges
from that of Spyroceras through Protokionoceras and_ finally
Kionoceras. The earliest stage, represented by a slightly flat-
tened silicifed individual expanding from 2 mm. to 6 mm. in 24

133 CLINTON CEPHALOPODS: FLOWER ial

mm., shows prominent longitudinal liree spaced four in a width
of 2 mm., crossed by slightly more prominent annuli which occur
five in a length equal to an adoral diameter of 5 mm, near the
adoral end of the specimen. The next stage, shown by an indi-
vidual 22 mm. long expanding from 6 mm. to 9 mm., shows the
longitudinal lire becoming more widely spaced, four occurring
in a width of 5 mm. at the adoral end. The annuli are reduced to
transverse ridges, fainter than the longitudinal ones and spaced
much more closely than before in relation to the diameter, occur-
ring eight in a length equal to an adoral diameter of 8 mm, In
addition, there appear at this stage fine longitudinal lire in the
interspaces between the stronger ridges, six or seven appearing
in an interspace.

The latest stage shows the longitudinal ridges becoming more
widely spaced and prominent, the areas between becoming slight-
ly concave. Only faint traces remain of the longitudinal lire,
which apparently become more numerous; the transverse ridges,
now as faint and nearly as frequent as the fine longitudinal
ridges, produce a subcancellate surface pattern.

The camerz are shown clearly only on one individual, which
is slightly flattened. Here four camer occur in a length equal
to the greater diameter of 17 mm.

Discussion.—The later stages of this species are comparable in
proportions with the known parts of Kionoceras rochesterense
Foerste and Kionoceras subcancellatum (Hall), both of the
Rochester shale. Kionocerasmutabile differs from rochesterense
in the presence of more prominent longitudinal ridges, and the
cevelopment of fine longitudinal and transverse markings in the
interspaces, From K. subcancellatum, it is distinguished by the
equal and uniform strength of the prominent longitudinal ridges.

Types.—Syntypes, Buffalo Museum of Science, Nos. E1070,
F-10745, (three specimens) a-c.

Occurrence.—In the silicious bands of the Clinton, apparently

Irondequoit limestone ; Gasport and Lockport, New York.
Kionoceras perlineatum Flower, n. sp. Plate 2, fig. 6

The phragmocone of this species is unknown. The type con-
sists of a portion of a living chamber 62 mm. in length and 32

12 BuLueTiIn 105 134

nm. in basal diameter . The surface differs from that of K. sub-
cancellatum (Hall) of the overlying Rochester shale in possess-
ing an extra series of lines. In K. subcancellatum (Hall) only
two series are developed. While the spacing of these lines is very
similar in the two species, K. perlineatum possesses in addition a
third series of alternating longitudinal lire, weaker than the first
two pairs. No transverse markings are developed. The internal
mold is faintly constricted, producing an obscurely annulated ap-
pearance.

Discussion.—Ot the described species the one most similar to
K. perlineatum is probably Kionoceras strix (Hall and Whitfield)
of the Liston Creek limestone, of Clinton age, of northern Indiana.
In this species, which attains a much greater size than the frag-
ment at hand from the Irondequoit limestone, the surface may
possess three series of markings, which become progressively
weaker, or the second and third may be subequal in strength.

In view of the lack of the phragmocone, the exact relationship
of this species cannot be determined. K. strix, which is probably
the most similar American form, is a Virgoceras, judging by its
internal structure. No doubt a new generic name will have to be
proposed for such longitudinally marked forms. The internal
structure of the nearest neighbor, Kionoceras subcancellatum
(Hall) of the Rechester shale of New York, is unknown. The
species 1s known entirely from flattened individuals. K. subcan-
cellatum shows very similar spacing of the primary and second-
ary longitudinal lire, but lacks the third and finest series.

The ornament is faintly reminiscent of that of Virgoceras can-
cellatum Flower (1939, p. 162) in the series of alternating longi-
tudinal markings, but there is no trace of the fine transverse
markings which characterize that species. Whether or not there
is any relationship cannot be determined until the phragmocone
of this species has been studied.

T ype.—-Holotype, Buffalo Museum of Science, No. E10788.

Occurrence.—From the Irondequoit limestone, Clinton group,
Middle Silurian, from Gasport, New York.

Genus DAWSONOCERAS Hyatt

Dawsonoceras Hyatt, 1884, Proce. Boston Soc. Nat. Hist., vol. 2? Denon
Hyatt, in Zittel, 1900, Eastman Textb. Paleont., vol. 1. 1st CXS. Joke Gullfsic
1913, 2d ed., p. 599; 1927, 3d ed., p. 599; Clarke and Ruedemann, 1903,

i135) \LINTON CEPHALOPODS: FLOWER 13

New York State Mus., Mem. 5, p. 82; Grabau and Shimer, 1510, North
American Index Fossils, vol. 2, p. 58; Ioers.e, 1924, Denison Univ.
Bull., Sei. uab., Jour., vol. £0, p. 225; Foerste, 1928, ibid., vol. 23
p- 26.

Cedarvilloceras Shimizu and Obata, 1935, Jour. Shanghai Sci. Inst., see.

» )

2, vol. 2, Pp. o.

?

Conch orthoceraconic, sometimes very slightly curved, with

aight transverse sutures. The siphuncle is only slightly eccen-
tric, orthochoanitic, with annulosiphonate deposits. Cameree
with mural deposits. The shell bears conspicuous annuli and
transverse surface markings which typically consist of scalloped
tranverse lire, Ornamentation is variable, longitudinal lire of
secondary nature may appear, again the festoons may become
vestigial, as may the annul.

Discusion.—Dawsonoceras is a highly characteristic Silurian
genus, being present in the Middle Silurian of Europe and also
extending into both the Lower and the Upper Silurian of Amer-
ica.

Shimizu and Obata have proposed a new genus, Cedarvillo-
ceras, based upon Dawsonoceras nodocostatum (McChesney).
So gradual is the development of nodes and longitudinal lire
from the transverse festooned liree that no line can be drawn be-
tween this genus and typical Dawsonoceras. Recognition of the
genus serves no useful stratigraphic purpose and is opposed by
the evidence of the close interrelationships existing among the
various species involved. Therefore Cedarvilloceras is here re-
garded as a synonym of Dawsonoceras.

Formerly, only one species of Dawsonoceras was recognized
in America, and this was considered conspecific with the Euro-
pean Silurian Dawsonoceras annulatum (Sowerby). An Ameri-
can species was later separated as a variety, D. annulatwm var.
americanum, which was subsequently given specific rank by
Foerste (1928). Savage (1917, p. 156, pl. 9, fig. 22) described
the only known Lower Silurian species, Dawsonoceras tenuiline-
atum, which approaches, in its surface features, the simple pat-
tern popularly considered characteristic of Cycloceras. Foerste
(1928) distinguished a number of other species of Dawsonoceras
which range throughout the Middle Silurian. Specific criteria
have been based almost entirely upon the details of the surface

14 BuLLEeTIN 105 136

features of the shell. This limitation is essentially the result of
the fragmentary nature and frequently poor preservation of the
material and can be remedied only by a careful monographic
treatment of the genus on the basis of much better material than
is available at present. However, a brief review of the species
serves to show that, inadequate as our knowledge is, considerable
variation is evident in the recognized species as developed in var-
ious formations and localities, and that the recognized species
are not so sharply set off from one another as one might wish.

Dawsonoceras americanum is discussed below, and specimens
from the Irondequoit limestone are figured and described. The
typical form is that found in the Rochester shales, where individ-
uals are found in a flattened state. The greater number of Daw-
sonoceras of the Osgood limestone of Indiana appear to be iden-
tical, though with them there is associated an early form of D.
nodocostatum. Ina large suite of specimens from the Waldron
shale of Tennessee, it is possible to recognize this species by the
evenly spaced and relatively distant transverse markings, though
some individuals show a tendency for the liree to become crowded
at the crests of the annuli. This feature is characteristic of Daw-
sonoceras annulatum (Sowerby) of the Silurian of Europe, but
none of the Waldron specimens which I have seen show the
crowding developed as strongly as 1s shown in the specimen from
the Wenlock of England figured by Foerste (1928, pl. 5, figs.
Ia-b).

In the Waldron and Osgood, there are discernible two types
of D. americanum, one of which has the surface markings slight-
ly more closely spaced than the other. The differences do nct
appear to be great enough to serve as a basis for the designation
of, these forms as distant species or even varieties at the present
time, for enough material has not been gathered to preclude the
possibility of intergradation in different parts of the same indi-
vidual. However, it is interesting to note that there is an indi-
cation of variability here which points toward the different spe-
cies which have been recognized from higher formations.

137 CLINTON CEPHALOPODS: FLOWER 15

Forms with very closely spaced transverse markings, which
tend to loose annuli and in which the festooning becomes ex-
tremely irregular, are present in the Osgood (Foerste, 1928, pl.
61, fig. 5) and are abundantly represented in the Waldron shale.
These forms resemble D. americanum in the early stages, and
there is demonstrable variability in the point at which the annuli
are reduced, and fine, rather rugose, transverse markings pre-
dominate; nevertheless, they appear distinct enough to be set
aside as a separate species for which the name Dawsonoceras
rugosum is here proposed. This stock can be traced higher in
the section, and the annuli are completely lost at a relatively early
stage in a form from the Racine dolomite here described as Daw-
sonoceras senescens, A representative of this form was described
by Foerste (1928, pl. 56, fig. 9) as Geisonoceras wauwatosense, a
species which has typically much more regular surface features.
Nevertheless, it is worth noting that in the ultimate development
of this stock the essential features of the genus Dawsonoceras have
been completely obliterated, and only the study of the interme-
diate Waldron species will show the actual relationship.

A second deviation from the stock of annulatum is character-
ized by the retention of regular festoons of transverse lire, but
the lire become more distantly spaced. This is represented by
Dawsonoceras graftonense Foerste (1928, p. 158, fig. 6) of the
Racine dolomite, and fragments of a closely similar form, but
one with even more distantly spaced lire, occur in the Laurel
limestone of southern Indiana.

Dawsonoceras hyatti Foerste is known only from portions of
relatively late stages of large individuals and is characterized by
broad rounded annulations and numerous finely festooned trans-
verse lire. The species was described from the “Lockport” of
Hamilton, Ontario. Foerste referred specimens from other lo-
calities to it, none of which appear to be quite identical in surface
features. Specimens from the Cedarville dolomite of Ohio
(Foerste, 1928, pl. 58, figs. 1, 2, 4, 5) have the annuli less broad-
ly rounded, and the transverse markings seem to be thickened at

16 cia LOETIN 105 138

the mile of each of the shallow arcs making up the character-
istic surfiace markings. Another specimen, this time from the
joilet limestone of Illinois (Icerste, 1928, pl. 59, fig. 2), is more
typical, but in the later part of the shell the festoons are lost.

D. snultilivatum (Foerste, 1928, p. 279, pl. 60, figs. 1-2) is the
mest Cistinctive form, bearing prominent longitudinal markings
Cceveloped at tne crest of the aligned festoons of the surface. It
can be distinguished from D. nodocostatum by the broader and
(letter annuli as well as by the more prominent longitudinal mark-
ings and the absence of nodes, features which are found to be
rather variable.

The nodose forms are very close to those bearing longitudinal
markings and are typified by D. bridgeportense and D. nodocos-
tatum. D. granti Foerste of the Barton beds (Foerste, 1928, p.
29, pl. 4, fig. 1, pl. 28, fig. 5), which are probably to be classed
as Rochester rather than Lockport, possesses marked longitudinal
ornament but is not nodose. The dominant Dawsonoceras of the
Liston Creek dolomite of northern Indiana is a form very close
to typical granti. D .nodocostatium is represented by fragments
from the Osgood limestone, and from the Laurel limestone,
both of southern Indiana. The form was described from the
Racine dolomite, where the species develops rather broader
annuli than usual, and a form with narrower annuli has been re-
ported by Foerste (1928, pl. 585, fig. 3) from the Cedarville dolo-
nute of Ohio. D. bridgeportense is quite similar to nodocostatum,
but has oblique annuli.

It is quite evident that the species, as now defined, are of little
stratigraphic value. While typical americanum is not developed
in the Lockport of New York or Ontario, and is apparently found
in pre-Lockport strata in Indiana, it is probably unsafe to regard
the form as confined to the Clinton. Further, many of the more
complex species with more specialized ornament patterns, such
as nodocostatum, are definitely known to make their appearance
well below the development of the typical Racine. The specimens
of the Guelph have not, as yet, been adequately studied. Foerste
reported D. hyatti from the Port Byron (Foerste, 1928, p. 274,
pl 48, figs. 2a-b), but the surface markings are not preserved and

139 CLINTON CEPHALOPODS: FLOWER ilt/

the annuli seem to be both much narrower and much lower than
is typical of the species.

Dawsonoceras americanum (Foord) Plate 1, fig. 6

Orthoceras annulatum Hall, 1843, Nat. Hist. of New York, Geology, vol.
4, p. 110, fig. 1; table of illustrations, No. 14, p. 17, fig. 1.

Orthoceras undulatwm Hall, 1852, Paleont. of New York, vol. 2, p. 295,
pl. 64, fig. la-f; pl. 65, fig. 3.

Orthoceras annulatum Roemer, 1860, Silurian fauna western Tennessee,
Breslau, p. 78, pl. 5, figs. 18a-b; Billings, 1866, Cat. Sil. Foss. Anti-
costi Geol. Surv. Canada, p. 83; Hall, 1868 (extras 1865), 20th Rep.
New York State Cab. Nat. Hist., p. 351, pl. 20 (11) figs. 4-6, (see.
expl. of plates, p. 393; rev. ed., 1870, p. 411, pl. 20, figs. 4-6; pl. 24,
figs. 2-4, p. 433; Hall and Whitfield, 1895, Geol. Surv. Ohio, Pal., vol.
2, p. 147, pl. 9, fig. 1; Whitfield, 1852, Geol. Surv. Wisconsin, vol. 4,
p- 298, pl. 19, fig. 1; Hall, 1882, llth Ann. Rep. Indiana Dep. Geol.
Nat. Res., p. 324; White., ibid., 1882, p. 358, pl. 38, fig. 1; Chamber-
lin, 1883, Geol. Wisconsin, vol. 1, p. 194; Whiteaves, 1884, Pal. Fos.,
Geol. Surv. Canada, vol. 3, pt. 1, p. 38; Leslie, 1889, Geol. Surv. Penn-
sylvania, Rep. Progr., 4, p. 542, figs.; Grabau 1901, Buffalo Soc. Na..
Sei., Bull. vol. 7, p. 215, fig. 147; New York State Mus., Bull. 45,
1901, p. 215, ‘fig. 147.

Orthoceras (Dawsonoceras) annula um Kindle and Breger, 1904, 28th
Rep. Dep. Geol. Nat. Res. Indiana, p. 472, pl. 19, figs. 3-4.

Orthoceras (Cycloceras) annulatum Foerste, 1899, Proce. Boston Soe. Nat.
Hist., vol. 24, p. 282, pl. 8, fig. 5.

Dawsonoceras annulatum Grabau and Shimer, 1910, North American In-
dex Fos., vol. 2, p. 58, figs. 1260, 1261.

Orthoceras (Dawsonoceras) annulatum var. americanum Kindle and
Breger, 1904, 28th Rep. Dep. Geol. Nat. Res. Indiana, p. 472.

Dawsonoceras annulatum var. americanum Clarke and Ruedemann, 1903,
New York State Mus., Mem. 5, p. 81, pl. 10, figs. 9-21; pl. 11, fig. 1;
Grabau and Shimer, 1910, North American Index Fos., vol. 2, p. 58;
Grabau, 1909, Michigan Geol. Surv., vol. 1, p. 196, pl. 28, fig. 8; pl.
29e tioy ie

Orthoceras annulatum var. americanum Foord, 1889, Cat. Fos. Ceph. Brit-
ish Mus., p. 56; Whiteaves, 1895, Pal. Fos., Geol. Surv. Canada, vol.
3, pl. 2, p. 101.

Dawsonoceras americanum Foerste, 1928, Denison Univ. Bull., Sei. Lab.
Jour., vol. 23, p. 34, p. 5, fig. 4; pl. 28, fig. 4; Foerste, 1928, ibid.,
WO, Za 15 BO, jolly Gl saker, 4},

Although Dawsonoceras americanum (Foord), formerly the
only species of Dawsonoceras recognized in the American Silur-
ian, has been considerably restricted by Foerste, it still remains
such a variable species that it is possible that more than one spe-
cies is actually involved. The type, as selected by Foerste (1928,
Pp. 35), is a specimen from the Rochester shale, and the Rochester
forms can therefore be taken as typical. Unfortunately, the
Rochester specimens are almost entirely flattened, and as a result
little more can be used for species differentiation than the surface

18 BuuuEtTIN 105 140

markings, which are somewhat variable even among specimens
from the Rochester shale. The two specimens described below
from the Irondequoit limestone appear to be identical with the
Rochester form. The smaller one is of particular interest, for it
is apparently the first unflattened representative which can be
assigned here with absolute certainty. It shows the original
section, condition of the phragmocone, and makes possible a
closer study of the surface features with reference to the shell
proportions.

Foerste figured a specimen from the Osgood limestone of In-
diana which appears to be identical with the Rochester form
(1928, pl. 5, figs 2-3). Some specimens from the Waldron shale
appear to be identical, also, though, curiously enough, typical
americanum has not been definitely established in the intermedi-
ate Laurel limestone.

Two specimens from the Irondequoit limestone appear to be
not only well within the bounds of this rather variable species,
but very similar to the type, which occurs in the overlying Roches-
ter shales,

One of these is a small, undistorted shell, 95 mm. in length,
expanding from 9 mm. to 16 mm. in a length of 90 mm. The
sutures are straight and transverse. Slightly less than three
camere occur in a length equal to an adoral diameter of 12 mm.
The siphuncle is less than half a millimeter off center at the apex.
The annuli are very faintly oblique, sloping apicad on the siphonal
side. The annuli are spaced three in a length equal to an adoral
diameter of 11 mm., and the same proportion is retained to the
latest portion of this specimen. Festooned transverse lire are
uniformly spaced, slightly accentuated at the crests of the annuli
but not crowded. Between six and seven lire occur in the space
between the crests of two annuli. The festooning is regular, about
eight occurring on one-half of the shell.

The other, a much larger specimen, is somewhat flattened, but
at a mean conchial diameter of 32 mm., five or six annuli occur
in a length equal to that adoral diameter, The transverse lire
are slightly more closely spaced, varying from eight to twelve in
the interval between the crests of two annuli.

141 CLINTON CEPHALOPODS: FLOWER 19

Figured specimens.—Buffalo Museum of Science, No. 10784.
Occurrence.—In the Irondequoit limestone of Lockport, New
York.

Dawsonoceras senescens Flower, n. sp.
Geisonoceras wauwatosense Foerste, 1928, Denison Univ. Bull. Sci. Lab.,
Jour., vol. 23, pl. 56, fig. 9.

Conch slender, with the annuli completely lost, at least in the
later stages. Transverse markings show a complete loss of fes-
tooning, but in spacing and the irregular appearance of thickened
liree they are identical with those of Dawsonoceras percostatum
Flower. The holotype expands from 14 mm. to 19 mm, in 40
mm, The coarser lire average from 7 to 11 in a length of 10 mm.

Discussion.—The type of this species, which was figured by
Foerste as Geisonoceras wauwatosene (Whitfield) differs from
that species widely in the kind of surface markings, having the
transverse markings closely and irregularly spaced, and lacking
longitudinal markings entirely. In spite of the loss of the annuli
and festooning, it is evident that this is the final expression of the
stock represented in earlier strata by Dawsonoceras percostatum.
In D. senescens practically all the features characteristic of Daw-
sonoceras are lost. Nevertheless its close similarity to D. percos-
tatum leaves little doubt 2s to the relationship and origin of this
form, and the erection of a new genus for this single anomalous
species does not seem to be necessary. So far as is known at the
present time, this species is the last member of the genetic line
characterized by closely spaced markings within the genus Daw-
sonoceras.

Type.—Holotype, Museum of Comparative Zoology, No. 2303C.

Occurrence.—From the Racine dolomite, Middle Silurian, of
Waumatosa, Wisconsin.

Genus CYRTORIZOCERAS Hyatt

Conch cyrtoconic compressed, rapidly expanding in contrast ’
to the slender cyrtoconic Ooceras. The early stages are normally
circular in section, but, relatively early, the greatest shell width

20 BULLETIN 105 142

appears dorsad of the center, and the height expands more rap-
idly than the width. On the mature living chamber, the lateral
outlines become faintly convex, contracting toward the aperture.
The aperture bears a hyponomic sinus which is usually clearly
marked. The sutures are straight and transverse in the earliest
stage, but in the adoral portion they tend to slope orad on the
venter. Lateral lobes are variable in their occurrence and de-
velopment, being best seen in the more strongly compressed spe-
cies and rarely developed in the broader forms. The siphuncle
is close to the venter. The segments in the genotype are described
by Foerste as narrowly fusiform. In the Silurian species the
segments are somewhat broader and are scalariform in vertical
section, No deposits are known in the siphuncle or camere.

Discussion.—At the present time there seems to be insufficient

justification for the separation of Ordovician and Silurian species.
Any differences in the outline of the siphuncle appear to be minor
and show too much variability in Silurian species to serve as a
good basis for distinction. The genus is a large one, rather vari-
able, and one which does not seem to be susceptible to further
division, particularly when the known Bohemian as well as the
American species are considered. It is very similar to the more
slender Richardsonoceras Foerste of the Ordovician and appears
to grade into Ooceras, both in form and surface features. Like-
wise the siphuncle seems to vary from slender segments, such as
are found in the Ordovician genotype, some Silurian species, and
the genus Ooceras, to broader segments, such as are found in
the American Silurian species described below. Further expan-
sion, of which there is evidence in some species, usually accom-
panied by a more compressed form, leads to, and apparently
grades into, the condition found in Oxygonioceras. Indeed, the
Silurian of Bohemia contains species, such as Oxygonioceras
simplex (Barrande, pl. 10, figs. 8-11), which are transitional, both
in outline and in the form of the siphuncle.

Lechritrochoceras and its allies appear to be more closely akin
to typical Ooceras than to Cyrtorizoceras, being generally more
slender in form and having suborthochoanitic siphuncular seg-
ments which vary in position from subcentral to ventral.

143 CLINTON CEPHALOPODS: FLOWER mil

The taxonomic position of cyrtochoanitic cyrtoceracones with
empty siphuncles is complex, and one to which there have been
no recent contributions. It is quite evident that the genera are
closely similar, varying somewhat in all features in section,
ornament, sutures, expansion, and form of siphuncle. From
the evidence of Barrande’s abundant illustrations, it seems un-
likely that any new morphological features await discovery. There
is apparently a group of cyrtochoanitic cyrtoceracones ranging
from slender to gibbous, probably becoming breviconic in part
and also trochoceran in their mode of growth. This group will
include several of Hyatt’s families: the Rizoceratide ; Oocera-
tidze ; and a new family which must be added for the reception of
suborthochoanitic trochoceroids. A problem, still awaiting fur-
ther information, is whether actinosiphonate genera, which dif-
fer but little from members of this group in other features, are
actually related or merely isomorphic.

Cyrtorizoceras reimanni Flower, n. sp. Plate 2, figs. 1-4

This is a moderately large Cyrtorizoceras of rather slender
form, moderately compressed section, and sutures which are
transverse laterally. Holotype expands from 8 mm. and 8 mm.
at apex, where the greatest width is dorsad of the center, to 34
mm. and 29 mm. at the base of the living chamber, in a ventral
length of 75 mm. and dorsal length of 52mm. Curvature is grad-
ual in the apical half of the phragmocone, the radius of curva-
ture of the venter being about 100 mm. ; Curvature increases orad
so that its radius becomes about 80 mm. The living chamber
becomes slightly straighter, more compressed, the lateral outlines
becoming slightly convex. Its ventral length is 42 mm., its dorsal
length, 38 mm. Height of aperture, 38 mm.-: estimated width,
32 mm.

The phragmocone contains about 16 camere, increasing from
3 mm. to 6 mm. in depth. The sutures are without lateral lobes.
The siphuncle, known from another specimen, is slightly convex,
scalariform in vertical outline; the dorsal neck, recumbent; the
free part of the connecting ring is in contact with the septum, then
becoming free and straight adapically but faintly concave in the
middle of more adoral segments, joining the preceding neck with
no area of adnation. The ventral meek as orthochoanitic; the

bo
bo

BuLLETIN 105 144

connecting ring convex in outline and broadly adnate to the pre-
ceding septum. As the sutures tend to become slightly oblique,
passing orad on the venture, the siphuncle is separated from
the venter by half its width, the septal foramen is markedly
oblique, giving the siphuncular segments a most peculiar aspect.
No deposits are known in either camerz or siphuncle.

A paratype shows proportions which are sufficiently different
from those of the holotype to suggest sexual dimorphism. The
apical portion of the shell is more rapidly expanded, and curva-
ture is more uniform over the phragmocone. The apex is blunt,
increasing to a circular condition of 7 mm. diameter in a length
of 4mm, Ina ventral length of 62 mm. and a dorsal length of
60 mm., the base of the living chamber is attained, where the
height is 33 mm., and the width 28mm. The living chamber has
a dorsal length of 36 mm. and a ventral length of 44 mm., attain-
ing a height of 36 mm. and a width of 29 mm. By the lateral con-
vexity contraction of the living chamber, both specimens are
mature.

The surface of the shell bears transverse lire and striz, often
quite faint, but indicating the presence of a hyponomic sinus on
the venter in every instance. The details of the ornament vary
among individuals and also among parts of the same individual,
those of the paratype illustrated being usually coarse.

Discussion.—An attempt to draw any telling comparisons be-
tween this and other species of Cyrtorizoceras has not been very
successful. It belongs to a group of species in which the section
is only moderately compressed, the compressed aspect being large-
ly due to the occurrence of the greatest width of the shell well
dorsad of the center and to the narrower condition of the venter
than of the dorsum, Such species have been known abundantly
in the Middle Silurian of the east-central area. The Clinton spe-
cies 1s not closely similar in proportions or aspect to American
forms, but recalls more strikingly many of the compressed
cyrtoceracones of the Silurian of Bohemia, which are properly
referred to the genus Cyrtorizoceras also.

Types.—Buffalo Museum of Science, Holotype, No. Bro0785;
paratypes, :10785 (three specimens), E10787 (3 specimens in-
cluded).

145 CLINTON CEPHALOPODS: FLOWER 23
Cyrtorizoceras coralophilum Flower, n. sp. Plate 1, fig. 5

This is a moderately small species, only slightly curved adapi-
cally, and with the dorsum becoming straight over the mature
living chamber. The venter is uniformly curved, the radius of
curvature being 65 mm. The phragmocone expands from 22
mm, and 24 mm. to 25 mm. and 30 mm. in length of 25 mm.
Four subequal camerz occur in that length. The sutures rise
orad on the venter, but the lateral lobes are scarcely developed.
The siphuncle lies so close to the venter that its expanded por-
tion is in contact with th ventral wall. The living chamber ex-
pands from 25 mm. and 30 mm. to 30 mm. and 34 mm. 1n a ven-
tral length of 30 mm. Portions of the aperture are preserved.
The lateral outlines are slightly convex over the living chamber,
indicating a mature condition, although the last camere are not
contracted. The surface bears fine, rather irregular, transverse
liree and striz, which preserve the outline of the hyponomis sinus
on the venter.

Discussion.—The broad section, the poor development of the
lateral lobes of the sutures, and the straight dorsum should serve
to distinguish this from all other species of Cyrtorizoceras.

Type.—Holotype, Buffalo Museum of Science, No. E10786.

Occurrence.—From a bioherm in the Irondequoit limestone
at Lockport, New York.

Cyrtorizoceras fili°erum Flower, n. sp. Plate 1, fig. 8

Conch relatively gibbous, expanding from a faintly compressed
subcircular section of 13 mm. and 14 mm. to a strongly com-
pressed condition of 38 mm. and 30 mm., where dorsum and ven-
ter are about equally rounded in the length of the phragmocone,
which is 80 mm. ventrally and 20 mm. dorsally, with the radius
of curvature of the venter increasing from 25 mm. at the apical
third to 50 mm. at the adoral end. The living chamber has a
ventral length of about 60 mm., the aperture being incomplete at
that region; the dorsal length, 35 mm. The height of the aper-
ture is 50 mm.; the estimated width, 38 mm. As in other Cyrto-
rizoceras, the lateral outline becomes faintly convex on the ma-
ture living chamber.

The sutures are straight and transverse adapically, but adorally
they slope markedly orad on the ventral side, though without

24 ; BULLETIN 105 146

marked development of lateral lobes. The camere increase grad-
ually in depth, measuring 6 mm. at the adapical end and 9 mm.
at the adoral end of the phragmocone. The siphuncle is so close
to the venter that the expanded segments are in contact with the
ventral wall. In the plane of the septum, the foramen in 3 mm.
and siphuncle expands to 5 mm., with a length of 5 mm. The
outline of the segments is the same as in C. reimanni. As in that
species, there is no evidence of organic deposits in either the cam-
ere or the living chamber.

Discussion.—This species is readily distinguished from its asso-
ciate, C. reimanni, by its greater size, more rapid expansion, more
oblique septa, and the siphuncle which is closer to the ventral wall.
Forms of comparable proportions from the Silurian of America,
all of which are considerably younger, show much better develop-
ment of the lateral lobes of the sutures.

Type.—Holotype, Buffalo Museum of Science, No. E10806.

Occurrence.—In the Irondequoit limestone, Clinton group,
Middle Silurian, at Gasport, New York.

Genus LECHRITROCHOCERAS Foerste

Lechritrochoceras Foerste 1926, Denison Univ. Bull., Sei. Lab., Jour.,
vol. 21, p. 367, pl. 35, fig. 5; Poerste, 1930, ibid., vol. 25, p. 46.

This genus was erected originally for the reception of simple
trochoceroids with transverse but not longitudinal markings.
However, Foerste later referred to the genus those species with-
out transverse strize and lire which, by original definition, might
better be placed in Leurotrochoceras Foerste. He drew the gen-
eric boundary at another point, placing in Leurotrochoceras only
species which developed a strongly compressed section and a
siphuncle which lies at least halfway between the venter and the
center. Evidently in this case the disregard of the surface fea-
tures as generic criteria is a matter of convenience and of neces-
sity. The American species are largely preserved in dolomites,
and it is not absolutely certain whether fine transverse markings
might have been present originally, but were destroyed in all
known specimens. It is further evident that the relationship be-
tween the genera is so close that the only justification for using
two generic names is one of convenience in handling a large num-
ber of species, a practice that is to be seriously questioned.

147 CLINTON CEPHALOPODS: FLOWER 25

Lechritrochoceras clintonense Flower, n. sp.
Plate 1, fig. 7; Plate 2, fig. 7

This is a small Lechritrochoceras, very slightly compressed in
section throughout. The conch attains little more than one volu-
tion, though neither of the two known specimens retains clear
gerontic features. In half a volution, the holotype expands from
4 mm. and 5 mm. to 9 mm. and 10 mm., in a ventral length of
35 mm. The living chamber follows, which describes a quarter
of a volution and expands to 15 mm. and 16 mm. in a ventral
length of 40 mm.

The sutures are straight and transverse. The camerz occur
about four to five in a length equal to an adoral diameter of 10
mm. The siphuncle lies slightly ventrad of the center of the
conch and is suborthochoanitic in outline. At the base of the liv-
ing chamber, it is t mm. in diameter and 3.5 mm. from the venter.

The surface bears rather narrow rounded costz separated by
wider concave interspaces. The fine lire and striz, usually seen
in Lechritrochoceras, are lacking. The ribs occur about five in a
length equal to an adoral diameter at diameters of 11 mm. and
15 mm. Adapically the ribs are very obscure and are probably
completely absent on the first quarter volution. The aperture
bears a broad hyponomic sinus, which is retained throughout, so
that all costae slope apicad on approaching the venter.

Discussion.—In the absence of fine surface markings, this spe-
cies is closer to Leurocycloceras than to Lechritrochoceras, but
in typical Leurotrochoceras, the section is strongly compressed
and the siphuncle lies much closer to the venter. All of these fea-
tures are exceedingly variable among species, however, and it is
very questionable whether hard and fast boundaries can be found
distinguishing these genera.

The species can be distinguished from many Lechritrocho-
ceras by the absence of lirze and the faintly compressed section.
L. waldronense (Hall) is known from specimens which are com-
pressed, though it might be questioned whether they were origin-
ally so, as all specimens are somewhat flattened. L. waldronense
has more closely spaced costae. The rapid expansion and the
completion of only one volution serve to distinguish this species

26 BULLETIN 105 148

from most of its relatives. L. notum (Hall) of the Racine dolo-
mite is somewhat similar in aspect, but describes one and one-half
volutions. L. waldronense (Hall) of the Waldron shale, L. ban-
nisteri (Hall) of the Racine dolomite, and L. notum of the Ra-
cine are most similar in proportions, being relatively rapid in
their expansion, but all have much more closely spaced coste

Types.—Syntypes, Buffalo Museum of Science, No. E10794
(2 specimens).

Occurrence.—Irondequoit limestone, Clinton group, Middle-
port. Nj Y.:

REFERENCES

Flower, R. Hi.
Revision and internal structure of Leurocycloceras, Amer. Jour.
Sci., vol. 239, No. 7, 1941, pp. 469-488, 3 pls.
Foerste, A. F.
American arctic and related cephalopods, Denison Univ. Bull.
Sci. Lab., Jour., vol. 23, 1928, pp. 1-110, pls. 1-29.
————— A restudy of American orthoconice Silurian cephalopods, Denison
Univ. Bull., Sci. Lab., Jour., vol. 23, 1928, pp. 236-320, pls.
48-75.
————— A restudy of some of the Ordovician and Silurian cephalopods
described by Hall, Denison Univ. Bull., Sei. Lab., Jour., vol.
23, 1928, pp. 173-230, pls. 40-47.
Hall, J.
Paleontology, New York State Geol. Sur., vol. 2, 1852.
Savage, T. E.
Stratigraphy and Paleontology of the Alexandrian series in
Illinois and Missouri, Illinois State Geol. Surv., Bull. 23, 1917.

PLATES

PEATE 1 (12)

28 BULLETIN 105 150
EXPLANATION OF PLATE I (12)
Figure Page
1-4. Kionoceras mutabile Flower, n. sp. ——--------------------_---_--__--_ 10
Four syntypes showing (1) most mature specimen known;
(2) a slightly earlier stage with better preserved mature
surface markings; (3) earliest stage known with annuli;
(4) intermediate stage with vestigial annuli. Figs. 1, 2, and
4, are No. E10745, Buffalo Museum of Science, from the
Irondequoit limestone at Lockport, New York. Fig. 3, No.
E10780, Gasport, New York.
5. Cyrtorizoceras coralophilum Flower, n. sp. pees 28
Holotype, lateral. Buffalo Museum of Science, No. E10886.
Irondequoit limestone, Gasport, N. Y.
6. Dawsonoceras americanum (Foord) ~~ eee NE ae - 7
Buffalo Museum of Science, No. E10784. Irondequoit lime-
stone, Lockport, N. Y.
7. Lechritrochoceras clintonense Flower, n. sp... BT AG
Syntype, Buffalo Museum of Science, No. £10794. Irondequoit
limestone, Middleport, N. Y.
8. Cyrtorizoceras filiferum Flower, n. sp. Ze
Holotype, lateral aspect. Buffalo Museum of Science, No.
£10806. Irondequoit limestone, Gasport, N. Y.
9. Leurocycloceras ringuebergi Flower, n. sp. __- 10

Buffalo Museum of Science, No. E10672. rondeauorr ee
stone, Lockport, N. Y.

Pu. 12, Vou. 27 Buu. AMER. PALEONT. No. 105, Pu. 1

nN
ar -
2
a

30 BULLETIN 105

I:XPLANATION OF PLATE 2 (13)

152

Figure Page

1-4. Cyrtorizoceras reimanni Flower, n. sp. _---..-----------------------------—----—-
(1) Paratype, lateral aspect; (2) holotype, lateral aspect;
(3) holotype, ventral aspect; (4) portion of siphuncle from
a second paratype. Buffalo Museum of Science, E10785,
(figs. 1-3). E10787 (fig. 4). Irondequoit limestone, Gasport,
IN(g: WE
5. Armenoceras subvertebratum Flower, n. sp. ~~~
Section of adoral end of holotype parallel to bedding. The
surface exposed is slightly oblique to the transverse plane
of the specimen, being nearer the venter on th right than
on the left. Buffalo Museum of Science, No. £1077. Ironde-
quoit limestone, Gasport, N. Y.
6. Kionoceras perlineatum Flower, n. sp. —~
Holotype, Buffalo Museum of Science, No. E10788. Ironde-
quoit limestone, Gasport, N. Y.
7. Lechritrochoceras clintonense Flower, n. sp. ~~ oe
Syntype, showing proportions of camerz. Buffalo Museum of
Science, No. E10794. Irondequoit limestone, Middleport,
INS X.-

21

bo
an

No. 105, Pu. 2

Buu. AMER. PALEONT.

Pu. 13, Vou. 27

* « } A 1 7
® i
ar) 1
f a
~
i
{
{=
1
@ +
i A i
i a

' _

‘oes
Be ge

: “aN

106

ale ee Phi Aa Ria cask
_ PALEONTOLOGICAL RESEARCH INSTITUTION
| Ithaca, New York -
3s a

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. [06

Tertiary and Quaternary Fossils from the
Burica Peninsula of Panama and Costa Rica

By

A. A. Olsson

December 25, 1942

Paleontological Research Institution
Ithaca, New York
WS Eas

1S, F6/

of Com,”
GP roca ie “
W4N 14 1943
LIBRARY

GONTENTS

Page

Foreword es See ae Sm ae te ee 9 ies ee eee ee 5
NMC CLO MMi Pak ck Pee, Se. te ee Seeiyee s yaw ee, me ee a Es 5)
Stratigraphy and paleontology ~~ pea Ele Sah 8 es ESS
The Armuelles formation (Olsson, 1942) FR RPE a pL ID ie Stee an: ee Ae 8
Fossils from the zone of unconformity at Punta de Piedras... 11
The Charco Azul formation (Olsson, 1942) (Pliocene)... 12
(Oven mee Atzeret lt 2 ce ole oo Ae a oe ld et dee Eee 15
CNC DCA Ay NUOUITS AY ve. Chew se teks ome We echt aden eee eas 16
IRTOWCIa AOA OTE tw) ware. nt We URE. eS Ser eed ae eee sie f 17
IMonmihwore@uelnadan erie ines see tne ee rs ese een ee eee ss 18
QuebradasRenitasy 2 Wee yeh eee ete fe Bee ae oP tes we eee 18

EV Omeiciye Nic Cabs) eect eae ee On een Rit eles nt ao eon N en Fete» 19

IRiow blanco. see Pa ni ig NY Ae SETS, GPE De ME te AR oes ea oe 20
Burica, sandstones (Olsson LOLA oy eee Le ote i AD hee ee 21
AVE ROTONCC Shee et cas eae eo teu te Tas Ries MANES Tas SLPS ES AU kat: geen 23
BV StemMabies CESGhEptigns: fee eh Oyen tars. Bie Mohs eee Clee Pees ees ae 23
Plates 83

TERTIARY AND QUATERNARY FOSSILS FROM THE
BURICA PENINSULA OF PANAMA AND COSTA RICA

By
A. A. Olsson

FOREWORD

In this paper,* the following new genera and subgenera are
proposed:

Genus Luciploma of Veneride

Subgenus Panacoma of Macoma Leach
Subgenus Buridrillia of Clathrodrillia Dall
Subgenus Charcolleria of Cancellaria Lamarek
Subgenus Longitrella of Mitrella Risso
Subgenus Cotonopsis of Strombina Méreh

All the new species described in this paper are from the Burica
Peninsula except:

Cancellaria (Bivetopsis) charapota, n. sp. Miocene of Ecuador
Cancellaria (Charcolleria) perdiciana, n. sp. Miocene of Colombia
Cancellaria colombiana, n. sp. Miocene of Colombia

Dalium ecuadoriana, n. sp. Oligocene of Ecuador

Dentalium (Fissidentalium) esmeraldum, u. sp. Oligocene of Eeuador

INTRODUCTION

The principal purpose of this paper is the description and il-
lustration of certain new species of mollusks of late Tertiary and
Pleistocene age from the Burica Peninsula of southwestern
Panama and southern Costa Rica. Most of this material was
collected by Mr. R. A. Terry during several years of extensive
geologic studies on the Burica Peninsula and adjoining areas.
Other collections were made by Mr. Terry and myself in 1938.
I am also deeply indebted to Mr. Mark Trafton Jr. of the United
Fruit Company, stationed at Puerto Armuelles, for much in-
teresting Pleistocene, as well as Recent, material, A few new
species of gasteropods from the Oligocene and Miocene of north-
ern Colombia and western Ecuador have been included because
of their special interest.

“Manuscript submitted, Oct. 1, 1942.

6 BULLETIN 106 158

The Burica Peninsula forms the southwestern corner of the
Republic of Panama and hence also the Pacific, or terminal, por-
tion of the international boundary with Costa Rica. The penin-
sula itself is about 20 miles long with an average width of about
5 miles. It is for the most part covered with forest and only
sparsely inhabited at a few places. In the north, where the penin-
sula widens and merges with the mainland, the interior portions
are very rugged, and high cliffs of igneous rocks border the
shore on the Costa Rican side. These heights give rise to a small
mountain peak in the interior, known as Pico de Burica, with
an elevation of about 700 meters. Immediately north of Pico de
Burica is a belt of low lands between 15 and 20 miles wide and
drained, in part, in Costa Rica by the Rio Coto flowing west-
ward into the Gulf of Dulce, and in Panama by the Rio Chiriqui
Viejo flowing southeast into the Bay of Charco Azul. The east
shore of the peninsula is washed by the waters of Charco Azul,
the deepest bay along the Panama south coast and the western
part of the greater Gulf of Chiriqui.

The geology of the Burica Peninsula has been rather extensive-
ly investigated by Mr. R. A. Terry in connection with his broad-
er regional studies in Panama. <A short discussion of certain
features of the geology of the region, accompanied by a sketch
map of the areal geology and depth soundings in the Bay of
Charco Azul, is given by Terry (1941) in his paper on “Sub-
marine Valleys off the Panamanian Coast.”

Pico de Burica, as well as the adjoining rugged parts of the
peninsula, is principally formed of hornblende andesite, the com-
mon igneous basement rock in Panama, locally overlain by, or
in fault block contact with, upper Eocene limestones. This zone
of basement outcrop is part of an old uplift or structural trend
along which are also located the older rocks exposed in the in-
terior of the Peninsula of Osa in southern Costa Rica and in the
island of Coiba off the coast of Veraguas. In a similar way, the
low lands between Pico de Burica and the interior highlands lie
in a parallel trough or geosyncline which also includes the pres-
ent Gulf of Dulce, the Bay of Charco Azul and the Gulf of
Chiriqui. This trough is filled with a thick section of normal

159 BuricA PENINSULA FOSSILS: OLSSON 7

Tertiary sediments, including Eocene, Oligocene and Miocene
beds of which exposures are found at David, Brenon and other
localities along the north side.

In most parts of Panama, where Eocene beds are known to
occur, they are normally overlain by thousands of feet of shales
of Oligocene and Miocene age. These formations are missing,
however, on the Burica Peninsula or the region immediately
south of Pico de Burica, although well developed in the Rio
Coto-Rio Chiriqui-Viejo syncline as previously noted. The Pho-
cene deposits of the peninsula overlap the older rocks of Pico
de Burica so that this outpost mountain was an island during the
formation of these beds. On the peninsula, the formational strike
is normally northwest and southeast with the regional dip towards
the north. Therefore, as we go south towards Burica Point, we
encounter progressively older beds in the following manner. In
the northern zone near Puerto Armuelles, the outcrops are of
Pleistocene age and consist, for the most part, of sands and
shales belonging to the Armuelles formation (Olsson, 1942).
Fossils are plentiful in certain horizons. The basal portion of
the Armuelles formation is formed by thick beds of conglomer-
ate well exposed at Punta de Piedra a few miles south of Puerto
Armuelles. This conglomerate marks an unconformity, and be-
neath it lies a great thickness of predominantly blue shales, rich
in small Foraminifera, known as the Charco Azul formation
(Olsson, 1942). This formation is of Pliocene age and outcrops
extensively on both sides of the peninsula and in many rivers
and quebradas in the interior. To the south, the lower beds of
the Charco Azul become increasingly tuffaceous and sandy and
grade down into the Burica sandstones (Olsson, 1942). These
sandy beds represent the lowest rocks exposed at the southern
end of the peninsula, Only a small fauna is known from the
Burica sandstones and their age cannot be definitely fixed. The
stratigraphy would seem to indicate that they belong to the same
sedimentary cycle as the Charco Azul and consequently are ten-
tatively referred to the uppermost Miocene or lowermost Plio-
cene. The thickness of the Burica sandstones is not known since

8 BULLETIN 106 160

they are only partly exposed, but both the Armuelles and Charco
Azul formations have a maximum thickness of about 4000 feet.
These formations have been strongly folded and faulted, and their
structure bevelled by erosion.

The Burica Peninsula is the most active seismic region in
present-day Panama, the continuation of the earth movements
which have so strongly deformed the sedimentary formations.
That the region has undergone great changes during the late
Tertiaries is clearly revealed by its geology. ‘The general north-
erly dip of the peninsular formations is partly an original de-
positional feature off an old land, the northern shoreline of which
was near Burica Point. In Miocene times, this Pacific land in-
cluded the peninsula as far north as the Rio Coto syncline, as
the general overlap of the Pliocene beds on basement rocks indi-
cate. The destruction of this land in the later Tertiary and
during the Pleistocene was accompanied by violent volcanic ac-
tivity, and consequently volcanic or tuffaceous materials become
increasingly more important as a sedimentary constituent towards
the south. The geology of the Burica Peninsula has an important
bearing on the Tertiary history of Panama and on the larger re-
gional problems dealing with the tectonic development of the
Pacific coast of Central America and northern South America.
A short discussion of the history of the region, based principally
on the submarine topography of Charco Azul, has been contrib-
uted by Terry. The common occurrence of many fossils with
deep-water characteristics, in the Pliocene formations in particu-
lar, is the most interesting feature of the entire fauna and fully
supports the geologic interpretation of great changes in the Pa-
cific region during the late Tertiary and Quaternary periods.

STRATIGRAPHY AND PALEONTOLOGY
THE ARMUELLES FORMATION (OLSSON, 1942)

This formation outcrops typically near Puerto Armuelles, and
good sections are found in most streams in the vicinity, such as
Rio Guanabanon, Rio Corotu, Quebrada Rabo de Puerco and
Rio San Bartolome. The beds consist principally of gray, well-
bedded, foraminiferal shales and soft sandstones. Some layers,
particularly near the base, are lignitic, containing leaves and
partially mineralized wood. The upper part of the formation is

161 BurIcA PENINSULA FOSSILS: OLSSON 9

generally quite sandy. These upper beds, outcropping in Que-
brada Rabo de Puerco and in Monte Verde Ravine, are rich
in fossil mollusks, and most of the known species were collected
from these horizons. The basal portion of the formation con-
tains at least two prominent conglomeratic horizons separated
by an interval of foraminiferal shale, their combined thickness
being about 600 feet. The conglomerate at the base is generally
strongly consolidated and is interbedded with blue sandstones.
This conglomerate forms Punta de Piedra on the shore of Charco
Azul about 4 miles south of Puerto Armuelles. At this place, it
contains boulders of andesite, red jasperoids and other igneous
rocks sometimes 6 feet or more in diameter. Its contact with
the underlying blue shales of the Charco Azul formation is an
unconformity, the upper layers of the Pliocene shales having
been deeply brecciated and the fissures filled with fossiliferous
sand. This zone of unconformity has yielded an exceptionally
interesting faunule of small mollusks.

The molluscan fauna of the Armuelles formation comprises
about 130 known species. It is a typical shallow-water as-
semblage, very similar to that living in near-shore waters along
the present south coast of Panama. A few species appear to be
new and are described in this paper. A few others, such as
Chione traftoni and Netia reversa magma, occur in the Pliocene
of Ecuador and elsewhere. The very high percentage of Recent
species in the Armuelles beds and its close relation to the pres-
ent fauna of Panama shows that the formation is not older than
the early Pleistocene.

Fossils from Rabo de Puerco and Monte Verde Ravine.—

Area (Scapharea) concinna Sby.

Arca (Seapharea) emarginata Sby.

Area (Cunearca) nux Sby.

Barbartia (Acar) illota Sby.

Netia reversa magma MacNeil

Pinna, sp.

Ostrea, sp.

Pecten dentatus Sby.

Pecten ventricosus Sby.

Plicatula dubia Hanley

Crenella ecuadoriana Pils. and Olss.
Anomia peruviana d’Orb,

BuLuETIn 106

Placuanomia panamensis, N. sp.

Pandora (Clidiophora), sp.

Thracia (Cyathodonta) dubiosa Dall

Thracia (Cyathodonta) undulata Con.
Euerassatella gibbosa Sby.

Crassinella, sp.

Chama corrugata Brod.

Chama (Echinochama) californica Dall
Diplodonta, sp.

Diplodonta (Felaniella), sp.

Cardium (Mexicardium) procerum Sby.

Cardium (Trachyeardium) senticosum Sby.
Cardium (Trigonioeardia) graniferum Brod. and Sby.
Cardium (Leevicardium) elenense Sby.
Cyclinella, sp.

Macrocallista squalida Sby.

Macrocallista traftoni, n. sp.

Pitar lenis Pilsbry and Lowe

Pitar (Lamelliconcha) concinna Sby.

Chione (Chionopsis) amathusia Phil.

Chione (Chionopsis) traftoni Pils. and Olss.
Chione (Lirophora) marie d’Orb.

Tellina (Eurytellina), sp.

Tellina (Eurytellina) panamanensis Li

Tellidora burnetti Brod. and Sby.

Macoma lamproleuca Pilsbry and Lowe

Macoma (Psammacoma) panamensis Dall
Macoma (Cymatoica) undulata Hanley

Semele levis Sby.

Semele jaramija Pils. and Olss.

Semele ef. californica Con.

Tagelus violaceus Carp.

Tagelus (Mesopleura) peruvianus Pils. and Olss.
Soleeurtus broggii Pils. and Olss.

Solecurtus galapaganus Dall

Mactra (Micromactra), sp.

Labiosa undulata Gould

Corbula biradiata Sby.

Panopea, sp.

Bullaria punctulata A. Adams.

Terebra (Terebra) robusta Hds.

Terebra (Strioterebrum) panamillata, n. sp.
Conus

Conus arcuatus Sby.

Conus virgatus Rve.

Conus tornatus Brod.

Polystira oxytropsis Sby.

Polystira, sp.

Turricula tuberculata Brod. and Sby.
Clathrodrillia inequistriata Li ;
Clathrodrillia (Carinodrillia) halis Dall
Crassispira tapoeana Dall
Nannodrillia nana Dall

Caneellaria (Caneellaria) ureeolata Hds.
Cancellaria (HBuelia) eremata Hds.

zebra Sby.—(Smaller spire than most Recent specimens)

162

163 BurIcA PENINSULA FOSSILS: OLSSON allt

Cancellaria (Euclia) cassidiformis Sby.
Oliva araneosa C. B. Adams.

Oliva polypasta Duclos

Olivella, sp.

Marginella sapotilla Hds.

Marginella minor Hds.

Lyria (Eneta) harpa Barnes

Latirus castaneus Rve.

Galeodea patula Brod.

Hanetia anomala Rve.

Hanetia pallida Brod. and Sby.
Colubraria, sp.

Cymatium weigmani Anton

Distorsio decussatus Val.

Kngina maura Sby.

Cantharus elegans Gray

Triumphis distorta Lam.

Nassa pagoda Rve.

Phos veraguensis Hds.

Metula amosi Vanatta

Columbella major Sby.

Cosmioconcha modesta Powis
Strombina recurva Sby.

Strombina gibberula Sby.

Murex recurvirostris Brod.

Phyllonotus radix Lam.

Thais biserialis Bly.

Semicassis centiquadratus Val.

Ficus decussata Wood

Cypreea, sp.

Strombus gracilior Sby.

Turritella tigrina Kiener
Arehitectonica granulata Lam.
Crepidula onyx Sby.

Crepidula aculeata Brod.

Crucibulum (Crucibulum) umbrella Desh. (rudis Brod.)
Crucibulum (Crucibulum) spinosum Sby.
Crucibulum (Dispotea) imbricatum Brod.
Calyptrea conica Brod.

Calyptrea mamillaris Brod.

Natica broderipiana Reclus

Natica macrochiensis Gmelin

Polinices (Polinices) uber Val.
Neritina, sp.

Cireulus occidentalis Pils. and Olss.
Dentalium (Fissidentalium) buricum, n. sp.

FOSSILS FROM THE ZONE OF UNCONFORMITY AT
PUNTA DE PIEDRA

The basal conglomerate of the Armuelles formation, outcrop-
ping at Punta de Piedra about 4 miles south of Puerto Armuelles,
lies unconformably upon the Charco Azul. The zone of uncon-

12 BULLETIN 106 164

formity is indicated, in part, by a brecciation of the Charco Azul
shales, with the blocks recemented by seams of fossiliferous
sand. From this sand filling, was obtained a rich assemblage of
small mollusks of which the following list is a partial determina-
tion. This fauna is probably Pleistocene and represents shells
washed into the fissures in the shale during the initial flooding or
transgression by the Pleistocene sea, although the overlying
Punta de Piedra conglomerates are unfossiliferous. A few spe-
cies from the Charco Azul shales may have become mixed during
the collecting and washing of the samples, but this mixing is
probably not important. Probably the most interesting species
in this faunule is Condylocardia panamensis, the first record of
this South Pacific genus in America:

Condylocardia panamensis, n. sp.

Nannodrillia nana Dall

Philbertia trichodes Dall (hirsutum de Folin)

Marginella minor C. B. Adams

Marginella margaritula C. B. Carp.

Hanetia elegans Dall

Nassa, sp.

Turbonilla (Strioturbonilla) aff. thyne Bartsch

Turbonilla (Pyrgiscus), several species

Triphoris, sp.

Triphoris alternatus C. B. Adams

Cecum cf. suave de Folin

Seila, sp.

Kumeta, sp.

Rissoina ef. lauree de Folin

Rissoina cf. gisna Bartsch

Rissoina ef. effusa Moreh

Alvania bartschi, n. sp.

Teinostoma, sp.
Cireulus, sp.

THE CHARCO AZUL FORMATION (OLSSON, 1942) (PLIOCENE)

At Punta de Piedra, south of Puerto Armuelles, the Pleistocene
conglomerates of the basal Armuelles formation is seen to be un-
derlain by a series of blue to black shales which outcrop in typical
form along the shores of Charco Azul nearly to Punta Burica.
This formation has been called the Charco Azul and referred to
the Pliocene mainly on the evidence of its fauna. The formation is
also present on the Costa Rican side of the peninsula, outcrop-

165 Burica PENINSULA FOSSILS: OLSSON 13

ping in many streams and along the shore. At the mouth of Que-
brada Pefitas, in the northern part of the peninsula on the Costa
Rican side, the base of the Charco Azul is formed by a coarse,
blue sandstone containing small concretionary nodules and seams
of conglomerate. This sandstone lies directly upon the basement
andesite. Its fossils are mostly near-shore forms, with such
types as Thais, Cantharus, Modiolus, as well as rock barnacles.
These basal beds are found at several other places in this zone as
well as in the interior of the peninsula and prove the strongly
transgressive character of the Pliocene sea in this region. The
main part of the Charco Azul, exposed along Quebrada Penitas,
is a foraminiferal shale containing abundant limestone concre-
tions, some of which have a tubular form. As usual, in shale for-
mations of this type, molluscan fossils are scattered or occur
only in a few, restricted horizons.

The typical exposures on the east coast of the Charco Azul be-
long to the upper part of the formation. They are rather soft,
black shales and, as indicated by their fossils, were deposited in
waters considerably deeper than the shales found along Quebrada
Penitas. Excellent outcrops of the lower and middle part of the
Pliocene beds are found along the southwest coast of the penin-
sula and at low tide can be closely examined for miles. These
beds, however, have a different facies development from the rocks
exposed at Charco Azul and along Quebrada Pefnitas in that they
are tuffaceous. Fossils are rare in these tuffaceous shales, the
commonest forms being scattered specimens of Fissidentalium
buricum and Buridrillia panarcia. The lower beds become in-
creasingly more sandy and grade down into the Burica sand-
stones proper. Although the separation is entirely artificial, the
base of the Charco Azul formation is placed at a point in the sec-
tion where sandstone beds predominate over the shale. Accord-
ing to Terry, the thickness of the Charco Azul is about 4000 feet. .

The molluscan fauna of the Charco Azul varies according to
the conditions under which these beds were formed, and, in order
to show these differences, the fauna from each of the principal
localities is listed separately. In the exposures at Charco Azul,
many of the commonest species have deep-water affinities. These

14 BULLETIN 106 166

shells are often white in color, translucent or of glassy lustre;
others, such as the turrids, show the effects of water corrosion.
These deep-water forms are associated with others of a purely
shallow-water habitat. Assuming that the topography of the
sea-bottom at Charco Azul in Pliocene times was more or less
similar to that prevailing along the present coast or that the
Charco Azul shales were deposited on a steeply sloping or shely-
ing bottom, considerable variation in depth would take place in
comparatively short distances. Under these conditions, shallow-
water or littoral shells might easily be washed into deep water
by currents and storms where they would become mixed with
other species which normally lived in the deeper waters. Our in-
formation on the distribution of the deep-water mollusks of the
Panama region is based principally on the dredging conducted by
the Albatross Expedition and reported upon by Dall (1908).
Many species found in the Charco Azul shales, such as the tur-
rids, naticids and others, have close affinities with species dredged
by the Albatross.in waters as deep as 1471 fathoms. It must be
noted that dredging stations are generally so few and at such
widely spaced stations that it is not possible to obtain a compre-
hensive conception of the composition and distribution of the
deep-water fauna. It is also true that most dredging expeditions
lave devoted their main efforts to very deep or very shallow
waters, leaving unexplored the far richer, intermediate zone,
lying between 100 and 400 fathoms. The shales at Charco Azul
vere probably deposited in this depth of water, an opinion also
advanced by Coryell and Mossman (1942) from their recent
studies on the Foraminifera of the Charco Azul shales.

In lithology, the Charco Azul shales, particularly along Que-
brada Penitas, are similar to the Uscari of northern Panama and
Costa Rica and the tuffaceous shaly facies near Burica Point to
the Esmeraldas of northern Ecuador, This similarity is further
accentuated by the occurrence of large Dentalium, Acila and by
some turrids. Closer inspection of the fauna, however, reveals
that the great majority of shells are closely related to Recent
species in the Panamic region, while the purely Miocene element
is relatively slight and restricted to a few forms, such as 4cila,

167 Burica PENINSULA Fosstus: OLSSON alts)

Antillophos and certain cones. Relations with the recently de-
scribed Pliocene of Ecuador are fairly intimate as illustrated by
the common occurrence of such distinctive species as Strombino-
phos loripanus Pils. and Olss., Nassa puntablancoenis Pils. and
Olss., Strombina ecuadoriana Pils. and Olss., Scapharca wheelert
Pils. and Olss. and Macoploma. Stratigraphically, the Charco
Azul is overlain by the Armuelles formations with its unmistak-
able Pleistocene fauna. For these reasons, I am referring the
Charco Azul directly to the Pliocene and correlating it broadly
with the Jama and Canoa formations of western Ecuador. Fu-
ture collecting will undoubtedly add many species to this very
rich and interesting fauna.
CHARCO AZUL

This locality is approximately to kilometers south of Puerto
Armuelles on the east coast. The following species are repre-
sented in our collections from this locality. Related species and
their depth occurrence are indicated in parenthesis.

Nucula iphigenia azulensis, n. var. (N. iphigenia Dall, Gulf of Panama,

259 fathoms.)

Nuculana (Jupiteria) chiriquiana, n. sp. (N. agapea Dall, Gulf of Pan-
ama, 1672 fathoms.)

Nuculana (Jupiteria) davidana, n. sp.

Yoldia (Orthoyoldia) quiba, n. sp. (Y. panamensis Dall, Gulf of Panama,
182-322 fathoms.)

Scapharca charcoazulensis, n. sp.

Pseudamusium terryi, n. sp. (P. panamensis Dall, Gulf of Panama; Gala-
pagos; Mexico, 141-855 fathoms.)

Lucina (Lucinoma) chiripanicus, n. sp. (L. heroicus Dall, L. equizonatus
Stearns. )

Macoma (Panacoma) chiriquiensis, n. sp.

Sanguinolaria azulensis, n. sp.

Corbula (Varicorbula) granti, n. sp.

Polystira panamensis, n. sp.

Fusiturricula woodringi, n. sp. (F. fusinella Dall, Gulf of Panama, 153
fa.; Mexico, 58 fathoms.)

Clathrodrillia (Buridrillia) panarica, n. sp.

Leucosyrinx nicoya, n. sp. (L. persimilis Dall, Gulf of Panama, 1020
fathoms.)

Leucosyrinz buricana, n. sp. (L. galapagana Dall, Galapagos, 634 -fa-
thoms. )

Ancistrosyring cedonulli reevei, n. var. (A. cedonulli Reeve, Gulf of Pan-
ama, 10-153 fathoms.)

Borsonella adamsi, n. sp. (B. agassizi Dall, Gulf of Panama, 1471 fa-
thoms. )

Borsonella harrisi, n. sp.

Pleurotomella (Phymorhynchus) agina, n. sp. (P. argeta Dall, Galapa-
gos, 812-855 fathoms.) Be eo Gia , Galapa

16 BULLETIN 106 168

Cancellaria (Cancellaria) penita, n. sp.

Hanetia (Fusinosteira) alternata Nelson

Strombinophos loripanus Pils. and Olss.

Nassa (Uzita) armuella, n. sp.

Nassa (Uzita) terryi, n. sp. (N. miser Dall, Gulf of Panama, Mexico,
182-322 fathoms.)

Strombina (Cotonopsis), sp.

Mitrella (Longitrella) vespertina, n. sp.

Epitonium (Ferminiscala) ferminianum Dall, (B. ferminianum Dall,
Panama, Gulf of California, 24-153 fathoms.)

Natica scethra burica, n. var. (N. scethra Dall, Gulf of Panama, 153
fathoms. )

Metula, sp.

Harpa, sp.

The most interesting feature of this fauna is the deep-water
characteristics shown by some species. It is perhaps best illus-
trated by the turrids, amongst which we have such normally deep-
water genera as Leucosyrinx, Borsonella, and Phymorhynchus.
The Recent species of these genera closely allied to forms from
the Charco Azul as indicated in the above list, are recorded from
depths of 600 to 1500 fathoms. It is quite possible that some
of these fossils are drift shells brought into somewhat shallower
waters by upwellings. An interesting occurrence at Charco Azul
is the Ancistrosyrinx cedonulli reevei. The Recent representa-
tive of this elegant shell was first dredged by Cumings in the
Bay of Panama at a depth of about 10 fathoms, the type being
an immature individual. It was later dredged in some abun-
dance by the Albatross Expedition in the same region at depths
ranging from 30 to 153 fathoms. Another striking member of
the faunal assemblage is Hanetia (Solenosteira) alternata Nelson.
This species was first described from the Tumbez beds of north-
ern Peru. Until the discovery of this species in Panama, Nel-
son’s types from Peru (preserved in the Peabody Museum at New
Haven) remained the only specimens known. It is probably a
species of intermediate depth range which may account for its
general rarity as a fossil.

QUEBRADA MELLISA

This stream flows into the Bay of Charco Azul about 1 kilo-
meter south of the last locality. The fossils, in the list below,
were collected by Terry from exposures along Quebrada Mellisa

169 Burica PENINSULA FossILs: OLSSON 17

about 314 miles upstream. The fauna, as may be seen, contains
a high percentage of Recent species.

Area (Seapharea) chareoazulensis, n. sp.
Ostrea megadon Hanley
Cardium (Fragum) magnificum (Desh.)
Dosinia (Dosinidia) grandis Nelson
Pitar (Lamelliconcha) mellisa, n. sp.
Chione (Chione) vaca, n. sp.

Chione (Lirophora) ebergenyi Bose
Chione (Lirophora) kelletti Hds.
Cardita laticostata Sby.

Conus areuatus vacuanus, n. subsp.
Crassispira, sp.

Turricula duleia, n. sp.

Turricula (Knefastia) andesita, n. sp.
Oliva angulata Lam.

Oliva (Agaronia) testacea Lam.
Marginella, n. sp.

Fusinus mellissus, n. sp.

Hanetia anomala burica, n. subsp.
Strombinophos loripanus, Pils. and Olss.
Phos (Antillophos) rutschi, n. sp.
Strombina recurva Sby.

Strombina fusiformis penita, n. subsp.
Phyllonotus brassica Lam.

Malea ringens Swains.

Ficus ventricosus Sby.

Architectonica nobilis Roeding

Natica broderipiana Recluz

RIO GUANABANON

This river flows into Charco Azul about 31% kilometers south
of Puerto Armuelles. Fossiliferous exposures of the Armuelles
formation occur in its lower courses. The following species be-
long to the Charco Azul formation and were collected by Terry
from exposures about 4 kilometers upstream from the mouth.

Nucula iphigenia azulensis, n. subsp.

Area (Cunearea) nux Sby.

Area (Argina) brevifrons Sby.

Periploma planiuseula Sby., var.

Phacoides liani Pilsbry

Cardium (Trigoniocardia) obovale Sby.
Chione (Lirophora) kelletti Hds.

Pitar (Lamelliconcha) anona, n. sp.
Terebra (Terebra) elena Pils. and Olss.
Terebra (Strioterebrum) aspera Hds.
Terebra (Strioterebrum) guanabana, n. sp.
Clathrodrillia (Buridrillia) panarica, n. sp.
Conus arcuatus vacuanus, n. subsp.

18 BULLETIN 106 170

Conus ef. patriceus Hds.

Nassa (Arcularia) puntablancoensis Pils. and Olss.
Strombinophos loripanus Pils. and Olss.

Phos (Antillophos) rutschi Pils. and Olss.

Metula pilsbryi, n. sp.

Strombina ecuadoriana Pils. and Olss.

Bursa nana jamanensis Pils. and Olss.

Turritella tigrina Kiener

MOUTH OF QUEBRADA PENITAS
This locality occurs on the ‘Costa Rican side of the peninsula
slightly south of the latitude of Puerto Armuelles. The fossils
were collected in the basal part of the Charco Azul formations
only a short distance above the basement andesite.

Modiolus ef. purpuratus Lam.
Euerassatella gibbosa Sby.

Pitar (Lamelliconcha) rosea Brod. and Sby.
Cardium (Mexicardia) procerum Sby.
Terebra (Strioterebrum) cracilenta Li
Conus areuatus vacuanus, n. subsp.
Conus regularis Sby.

Polystira, sp.

Crassispira, sp.

Turricula duleia, n. sp.

Turricula (Knefastia) andesita, n. sp.
Caneellaria (Caneellaria) penita, n. sp.
Caneellaria (Caneellaria) ventricosa Hds.
Cancellaria (Peruclia) bulbulus Sby.
Oliva spicata Rod.

Oliva (Agaronia) testacea Lam.
Strombina recurva Sby.

Strombina ecuadoriana Pils. and Olss.
Strombinophos loripanus Pils. and Olss.
Typhis (Talityphis) costaricensis, n. sp.
Thais ef. biserialis Blainville

Cantharus elegans Gray

Bursa nana jamanensis Pils. and Olss.
Distorsio decussatus Val.

Vitularia ef. salebrosa King

Natica broderipiana Recluz

Polinices (Polinices) ef. panamensis Recluz

QUEBRADA PENITAS
These fossils come from the shale beds lying about 300 feet
stratigraphically above the basal sandstones. The fauna occurs
rather sporatically ‘and good fossils are common only at a few
places.

Nuculana (Jupiteria) davidana, n. sp.
Acila isthmica burica, n. subsp.

lyst BurIcA PENINSULA FOSSILS: OLSSON 19

Area (Seapharea) wheeleri Pils. and Olss.
Area (Cunearea) esmeralda Pils. and Olss.
Periploma ef. stearnsi Dall

Tellina (Eurytellina) panamanensis Li
Tellina (Macaliopsis) frontera, n. sp.

Macoma (Macoploma) medioamericana, n. sp.
Corbula ovulata Sby. var.

Ringicula (Ringiculella) costaricensis, n. sp.
Clathrodrillia (Buridrillia) panarica, n. sp.
Clathrodrillia harrisi, n. sp.

Conus (Leptoconus) arcuatus vacuanus, n. subsp.
Conus (Leptoconus) cacuminatus Spieker
Cancellaria (Canecellaria) penita, n. sp.
Caneellaria (Chareolleria) terryi, n. sp.
Caneellaria (Calearata) peninsularis, n. sp.
Mitra cyclica, n. sp.

Latirus penitus, n. sp.

Hanetia (Fusinosteira) alternata Nelson
Tritiaria (?) ecuadoriana Pils. and Olss.
Nassa (Areularia) puntablancoensis Pils. and Olss.
Cymatophos galerus Pils. and Olss.

Phos (Antillophos) rutschi, n. sp.

Strombina fusiformis penita, n. subsp.

Murex recurvirostris Brod.

Malea ringens Swainson

RIO LA VACA
This locality is situated in the upper part of Rio La Vaca in
Costa Rica, about 20 kilometers N. 45° W. of Puerto Armuelles.
The collection was made by Mr. Terry.

Nuecula iphigenia azulensis, n. subsp.
Area (Scapharea) obesa Sby.

Area (Cunearea) nux Sby.

Area (Argina) brevifrons Sby.
Netia reversa magma MacNeil
Crenella ecuadoriana Pils. and Olss.
Placuanomia, sp.

Peecten tumbezensis d’Orb.
Periploma planiuscula Sby., var.
Periploma, undet. sp.

Kuerassatella gibbosa Sby.

Crassinella, sp.

Divaricella lueasana Dall and Ochsner
Cardium (Mexicardia) procerum Sby.
Pitar (Pitarella), n. sp.

Pitar (Lamelliconcha) concinna Sby.
Chione (Chione) ef. amathusia Philippi
Chione (Chione) vaca, n. sp.

Chione (Lirophora) marie d’Orb.
Chione (Lirophora) kelletti Hds.
Dosinia grandis Nelson

Maeroeallista, sp.

Strigilla, sp.

20) BULLETIN 106 172

Tellina (Eurytellina) ecuadoriana Pils. and Olss.
Chama (Echinochama) californica Dall
Tagelus (Mesopleura) peruvianus Pils. and Olss.
Labiosa undulata Gould

Corbula ovulata Sby.

Terebra (Terebra) robusta Hds.

Terebra (Terebra) lingualis Hds.

Terebra (Strioterebrum) aspera Hds.
Terebra (Strioterebrum) vaca, n. sp.

Terebra (Strioterebrum) cracilenta Li

Conus emarginatus Reeve

Conus areuatus vacuanus, n. subsp.

Conus pyriformis Reeve

Conus puncticulatus Hwass

Caneellaria (Cancellaria) ureeolata Hds.
Caneellaria (Euclia) pacifica Pils. and Olss.
Oliva araneosa Lam.

Marginella, sp.

Latirus, sp.

Nassa (Arcularia) puntablancoensis Pils. and Olss.
Cymatophos panamensis, n. sp.
Strombinophos loripanus Pils. and Olss.
Metula pilsbryi, n. sp.

Strombina ecuadoriana, n. sp.

Bursa nana jamanensis Pils. and Olss.
Distorsio decussatus Val.

Aesopus (Glyptesopus), sp.

Turritella tigrina Kiener

Architectonica nobilis Roeding

Crucibulum (Crucibulum) hispidium Brod.
Crepidula onyx Sby.

Polinices (Neverita) glauca Humboldt
Natica broderipiana Recluz

Cireulus, sp.

Dentalium, sp.

RIO BLANCO

Rio Blanco is a large stream flowing into the Bay of Charco
Azul about 6 kilometers northeast of Puerto Armuelles. The
following species of the Charco Azul formation were collected
by Terry from the headwaters of the north fork of the Rio Blanco
near the Costa Rican border. This locality les on the north-
eastern slopes of Pico de Burica about 18 kilometers northwest
of Puerto Armuelles.

Nuculana iphigenia azulensis, n. subsp.
Nuculana (Jupiteria) davidana, n. sp.
Acila isthmica burica, n. subsp.
Periploma planiuscula Sby. (large form)

u/s} BuricA PENINSULA FossIus: OLSSON 21

Cardium (Trigoniocardia) spiekeri Hanna and Israelsky
Pitar, sp.

Macoma (Macoploma) medioamericana, n. sp.
Corbula ovulata Sby.

Terebra luctuosa Hds.

Conus ef. patriceus Hds.

Conus regularis Sby.

Conus pyriformis Reeve

Cancellaria (Caneellaria) ef. decussata Hds.
Oliva venulata Lam.

Oliva (Agaronia) testacea Lam.

Olivella, sp.

Marginella sapotilla Hds.

Phos (Antillophos) rutschi, n. sp.

Nassa (Arecularia) puntablancoensis Pils. and Olss.
Columbella major Sby.

Strombina ecuadoriana Pils. and Olss.
Strombina recurva Sby.

Malea ringens Swainson

Cypropterina pustulata Lam.

Natiea broderipiana Reeluz

Polinices aff. reclusiana Deshayes

Polinices panamensis Recluz

BURICA SANDSTONES (OLSSON, 1942)

Excluding the upper Eocene limestones of the north portions
of the peninsula and always structurally associated with the base-
ment rocks, the oldest formation exposed on the peninsula
proper, is the Burica sandstones, These rocks form the south-
ern end of the peninsula and the small islands nearby. As pre-
viously indicated, the Burica sandstones are transitional with
the overlying tuffaceous shales of the lower Charco Azul, This
relationship suggests that they are the lower portion of the sedi-
mentary series of which the Charco Azul shales are the higher
and deeper water facies. The actual base of the Burica sand-
stones and the basement on which they rest, are not known. The
lowest beds exposed at the Point are certain coarse, gritty sand-
stones and pebbly conglomerates, but large boulders of a very
coarse conglomerate, derived from still lower beds, occur on
the beach. At Burica Point, we are evidently close to the base
of the sedimentary section and near the margins of an old land
which once laid in the Pacific to the south. The majority of the
pebbles in the conglomerates belong to a black andesite and they
may be well rounded or angular; others are quartzitic.

22 BULLETIN 106 174

Fossils are generally rare in the Burica sandstones except as
small fragments of shells which are scattered throughout the beds.
Our best collection of mollusks was obtained in the lowest beds
exposed at Burica Point, the fossils occurring in a small pebbly
conglomerate interbedded with blue sandstones. The common-
est fossils in this horizon are the shells of Calyptogena, both as
closed and free valves. With them were associated Thyasira, So-
lemya and most of the species listed below. The type of
Solemya burica was nearly perfect when found with both
valves tightly closed. The other specimen of Solemya likewise
had both valves closed, but it is rather poorly preserved. The
other forms are ordinary shallow-water types and many are badly
broken and worn. The fauna of the Burica sandstones, as repre-
sented in our collection, is as follows:

Dentalium (Fissidentalium) buricum, n. sp.

Terebra (Strioterebrum), sp. (A large species but represented by frag-
ments only.)

Architectonica, sp. (Poorly preserved.)

Caneellaria, sp.

Hanetia pelicana, n. sp.

Cantharus amyecus n. sp.

Phos (Antillophos) gatunensis Toula

Fusinus, sp.

Siphonalia?

Turritella ef. gatunensis Conrad

Polinices, sp.

Nucula iphigenia Dall group.

Area, (A large, thick-shelled species, badly worn.)

Pecten, cast only (Perhaps P. tumbezensis d’Orb.)

Chione (Chione) araneosa, n. sp.

Chione, sp.

Luciploma panamensis, n. sp.

Thyasira bisecta Conrad

Solemya burica, n. sp.

The fauna of the Burica sandstones, as far as known from
rather meager collections, appears to be, in the main, distinct
from that in the overlying beds, The presence of Fissidentalium
buricum and Nucula iphigenia show that these beds are probably
not a great deal older than the tuffaceous shales of the Lower
Charco Azul. Relations with the Miocene is indicated by the
presence of Phos gatunensis and Turritella cf. gatunensis. These
two species are represented each by a single imperfect specimen.
Hence their identification is somewhat questionable. Until

i175} Burica PENINSULA Fossitus: OLSSON 23

the paleontology of the Burica sandstones is better known,
the age of these beds is tentatively considered as lower Pliocene
or uppermost Miocene.

REFERENCES

Coryell, H. N., and Mossman, R. W.

Foraminifera from the Charco Azul formation, Pliocene, of
Panama, Jour. Paleont., vol. 16, No. 2, 1942, pp. 233-246.

Dall, W. H. f
The Mollusca and the Brachiopoda (Albatross Rept.), Bull.
Mus. Comp. Zool., vol. 43, No. 6, 1908.

Olsson, A. A.
Tertiary deposits of northwestern South America and Panama.,
Proe. Highth Amer. Sei. Congress, vol. 4, Geol. Sciences, 1942,
pp. 248-250.

Terry, R. A.
Notes on submarine valleys off the Panamanian Coast,
Geog. Review, vol. 31, No. 3, 1941, pp. 377-384.

SYSTEMATIC. DESCRIPTIONS
Class PELECYPODA
Order PRIONODESMACEA
Family SOLEMYIDA®

Genus SOLEMYA Lamarck

Subgenus ACHARAX Dall
Solemya (Acharax) burica, n. sp. Pilater 2, tres a
The shell is large, rather solid for the genus, broadly elongated
in form and strongly rayed; anterior side wider than the pos-
terior and, originally, probably about 3 times as long; dorsal and
ventral margins parallel, shape of the two extremities not known
except through inference from the course of the lines of growth;
the surface is marked with strong, rayed bands which extend
from the beaks toward the ventral margins, defined by grooves;
these rays have the appearance of being alternately raised and
depressed with respect to each other; on the anterior submar-
gins, there are 5, raised rays, separated from each other by wide
furrows, nearly as wide as the rays themselves; they are fol-
lowed by 15 or 16 rays, separated only by grooves which cover
the middle of the valves (where they are widest) and the adja-

24 BULLETIN 106 176

cent parts of the posterior side, leaving the submargin itself
nearly smooth; the ligament is external, its remains forming a
knoblike mass behind the beaks.

Length of fragment, 58 mm.; height, 47 mm. ; diameter, 36 mm.

The type is a fragment, measuring about 60 mm. in length. It
shows the middle portion of both valves originally closed, and
filled with a pebbly sandstone matrix. The original length of the
perfect shell is estimated as about 115 mm. The substance of
the shell is fairly thick, about 2 to 3 mm, near the dorsal mar-
gin. Along the anterior-dorsal margin is a knoblike mass which
appears to be the remains of a wholly external ligament. Dall!
records 2 species of Acharax in the Recent Panamic fauna, both
from deep water, (S. agassizii Dall and S. johnsoni Dall) but
which differ from the fossil by their longer form and by their
sculpture. S. ventricosa Conrad, from the Oligocene and Mio-
cene beds of Oregon and Washington, seems nearer to A. agas-
sizw Dall of the Recent fauna than to our fossil. The species of
Solemya found in the Oligocene of Peru are likewise quite dif-
herent

Type.—Paleontological Research Institution, No. 4076,

Occurrence.—Burica sandstones, Burica Point.

Family NUCULIDA

Genus NUCULA Lamarck
Nucula iphigenia azulensis, n. subsp. Plate 4..fiesarcaroeee
ef. Nucula iphigenia Dall, 1895, Proce. U. S. Nat. Mus., vol. 18, p. 15.
ef. Nucula iphigenia Dall, 1908, Bull. Mus. Comp. Zool. vol. 43, p. 369,
pi nos: 14:

Shell large, solid, moderately convex; beaks opisthogyrate,
placed at the posterior one-third; the anterior end is produced
and is only a little more rounded than the posterior; surface of
the shell is smooth over the larger part, but with a series of fine,
narrow, irregular wrinkles present on the umbos but which fade
out and are replaced elsewhere by fine radial lines which are a
part of the internal-rayed structure of the shell itself; lunule nar-
row, linear; posterior area flattened except at the valve margins

1 Dall, W. H.: The Albatross Report, Bull. Mus. Comp. Zo6l., vol. 43,
No. 6, 1908, p. 364. Additional notes on Dall’s specimens are given by

Woodring, Lower Pliocene mollusks and echinoids from the Los Angeles
Basin, U. S. Geol. Survey, Prof. Paper, 190, 1938, p. 27 .

177 BuricA PENINSULA FOSSILS: OLSSON 25

which are elevated or slightly arched; the escutcheon is weakly
defined by a change in sculpture or the abrupt ending of the con-
centric wrinkles; interior brilliantly nacreous with a strong pal-
lial line connecting the muscle scars; margins of the valve coarse-
ly crenulated ; hinge has a large, obliquely set chondrophore ; and
has approximately 15 teeth in the posterior set and 28 in the an-
terior.

Length, 34 mm; height, 23.5 mm.; semidiameter, 7 mm.

iseneth, 31 mm. ; height, 21 nim. ; diameter, 13-5 mm.

Our shell, although related to Dall’s species, differs in being
less [phigenia-like in form, the anterior extremity being more
pointed and the posterior side more narrowly rounded. Dall’s
specimens were dredged from 259 fathoms of water in the Gulf of
Panama.

Type.—Paleontological Research Institution, No. 4074; other
specimen, No. 4075.

Occurrence.—Charco Azul.

Genus ACILA H. and A. Adams
Acila isthmica burica, n. subsp. Plate in fiese coos

Shell subovate, the posterior side 3 to 4 times the length of the
anterior, the beaks placed at the posterior three-fourths; the
sculpture consists generally of a single or primary bifurcation
which extends from the beaks obliquely backwards to the middle
line of the ventral margin, but in some specimens a secondary
bifurcation is present in the rostral sinus; the sculpture is gener-
ally normal in character in shells up to about 17 mm. in height
but in larger examples, the sculpture of the ventral area becomes
more or less crowded, discontinuous and often with many small
bifurcations as well as a crowding of the lines of growth in a
coarse manner; escutcheon and lunule absent or very poorly de-
fined; the dorsal area is sculptured with the continuation of the
ends of the ribs which in the younger shells extend to the hinge
margin but in the older ones is replaced by a zone of crowded
lines; in some specimens, the deep, interspaces between the ribs
is crossed by a series of fine, close, elevated, concentric threads.

Length, 32 mm.; height, 24 mm.; diameter, 15.5 mm,

26 BULLETIN 106 178

Length, 29 mm.; height, 20.5 mm.; diameter, 15 mm.
ally smaller and more trigonal in shape, the beaks being situated
less posteriorly than in this form. A lunule and escutcheon is
also generally present, sculptured similarly to the rest of the
dorsal margin as may be seen in the figures of A. isthmica given by
Schenck. On A. burica, a lunule and escutcheon seem to be
absent and the sculpture of the dorsal area is simpler.

It is of interest to record a species of Acila in Panama from
formations younger than the Gatun. Schenck has given the range
of Acila isthmica as occurring throughout the Miocene but this
extended range is not based on any records of the species in beds
of upper Miocene age. In Panama, typical 4. isthmica is known
only from the Gatun, the original specimens coming from the
rock excavated during the construction of the locks or from the
quarries to the east of the Chagres Spillway. This horizon be-
longs to the lower beds of the Gatun formation. Acila isthmica
is also found in the Las Perdices shales near Puerto Colombia in
northern Colombia. As first shown by Anderson* and later by
Olsson,® the Las Perdices horizon is much older than the true
Gatun and is correlated with the Upper Uscari of Costa Rica.
The known range of typical 4. isthmica in Panama and Colombia
15 therefore in the lower and middle Miocene.

T'ype.—Paleontological Research Institution, No. 4077; other
specimen, No. 4078.

Occurrence.—Quebrada Penitas, Costa Rica.

Family NUCULANIDZE
Genus YOLDIA Moller

Subgenus ORTHOYOLDIA Verrill
Yoldia (Orthoyoldia) quiba, n. sp. Plate 3, figs. 5

Shell of medium size, equivalve, inequilateral, the two ends of

In typical 4. isthmica Brown and Pilsbry,? the shell is gener-
2 Brown, A., and Pilsbry, H. A.: Proe. Acad. Nat. Sei. Phila., vol.
63, 1911, pp. 361, 362, pl. 27, figs. 11 192.

8 Schenck, H. G.: Nuculid bivalves of the genus Acila, Geol. Soe. of
America, Special Paper No. 4, 1930, 5) tii oly AM asters TL, BY By (a.

t Anderson, F. M.: Marine Miocene and related deposits of
Colombia, Proc. Calif. Acad. Sci., 4th series, vol. 18, 1929, p. 91.

,

north

6 Olsson, A. A.: The Peruvian Miocene, Bull. Amer. Paleont.. vol. 19,
1932, p. 39. See also note by Hedberg in Schenck, Nuculid pele cypods of
the genus Acila in the Tertiary of Venezuela, northern Colombia and Trini-
dad,, S“clogee Helvetia; vol. 28, No. 2, 1935, p. 904 (footnote).

179 BuricA PENINSULA FossIus: OLSSON 27

nearly equal length but with the posterior side shghtly narrower
and bluntly pointed at the end; umbos low, wide, nearly centrally
located with the small, scarcely coiled beaks touching each other ;
surface smooth, polished and ornamented in the middle zone by
strong, regular, concentric lines; escutcheon narrowly linear, de-
fined by a slightly elevated ridge; lunule similar but wider an-
teriorly ; ligament apparently wholly internal.

Length, 27 mm.; height, 14 mm.; diameter, 8 mm.

This species is perhaps related to Dall’s® unfigured Orthoyoldia
panamensis, described from the Bay of Panama, and dredged
from a depth of 322 fathoms. The measurements of O. pana-
mensis indicate a much smaller shell than the fossil.

Type.—Paleontological Research Institution, No. 4079.

Occurrence.—Charco Azul.

Genus NUCULANA Link
Subgenus JUPITERIA Bellardi

Nuculana (Jupiteria) chiriquiana, n. sp. Plate 1, fig. 7

Shell of medium size, plump and rather finely sculptured; the
beaks are nearly central or situated a little posterior of the mid-
dle; posterior side comparatively short, pointed at the end, the
anterior side only a little wider, narrowly rounded at the end;
posterior-dorsal area widely lanceolate, finely sculptured and
limited by a foldlike ridge from the rest of the surface; lunule
present, narrowly lanceolate, depressed with two limiting folds
on the side; surface sculptured with fine, regular, concentric
ridges separated from each other by deeply incised lines; these
ridges are of nearly equal strength over the general surface of
the shell but become finer on the umbos and coarser on the pos-
terior-dorsal area since there they represent the continuation of
each 3d or 4th ridge only ; interior deep, smooth, glassy with well-
marked muscle scars; pallial line faint, with a small, hardly vis-
able pallial sinus; margins entire; resiliary pit deep, directly un-
der the beaks, separating about 26 teeth in the anterior set and
18-20 in the posterior set.

6 Dall, W. H.: The Albatross Report, Bull, Mus. Comp. Zo6l., vol. 43,
IN, (@ UO, Th, etsi0),

28 BuLLETIN 106 180

Length, 20 mm.; height, 11.5 mm.; semidiameter, 5 mm.

This species has some resemblance to Dall’s Leda agapea from
the Gulf of Panama but has a shorter and narrower, posterior
side.

Type.—Paleontological Research Institution, No. 4080.

Occurrence.—Charco Azul.

Nuculana (Jupiteria) davidana, n. sp. Plate 1, fig. 3

Shell large, plump, with the small beaks placed nearly central
and closely adjacent; posterior end, narrowly produced, pointed,
the anterior side wider and rounded; ventral margin rounded
but bulging a little just anterior of the middle; posterior-dorsal
area lanceolate, flattened but with a small rise or bulge in the
middle; no lunule; sculpture consists of strong, concentric ribs
which are fairly large and regular, decreasing in size towards
the beaks; the ribs are separated by wide grooves; surface of
the shell, under a glass, may appear smooth, porcellaneous or
there may be a series of small, concentric lines covering both
the ribs and the interspaces ; the posterior-dorsal area sculptured
similarly with riblets but which are smaller and lie parallel to
the hinge line; hinge not exposed on the type specimen but in an-
other fragmentary shell, the posterior set of teeth number about
20.

Length, 27 mm.; height, 14 mm.; diameter, 12 mm.

The type is a complete shell of both valves, closed so that the
interior is not exposed. Another fragmentary specimen is rep-
resented by a broken left valve showing only the posterior side
of the hinge. This valve has a coarser sculpture and has about
20 teeth in the posterior set. The species resembles the Leda
balboe Brown and Pilsbury* of Gatun but is larger and more
coarsely sculptured. Nuculana gibbosa Sowerby, in the Recent
fauna is also similar but is even larger and has a finer sculpture.

Type.—Paleontological Research Institution, No. 4o81.

Occurrence.—Charco Azul.

7 Brown, A., and Pilsbry, H. A.: Proe. Acad. Nat. Sci. Phila., vol. 63

2
LOT ps B62, pl. 27, fig. 8. ’

181 Burica PENINSULA FOSSILS: OLSSON 29

Family ARCIDA®
Genus ARCA Linné
Subgenus SCAPHARCA Gray

Arca (Scapharca) charcoazulensis, n. sp. Plate 3, figs. 7, 8

Form transversely elongate, the dorsal and ventral margins
nearly parallel, the posterior side strongly oblique and the shell
moderately thin in texture; the right valve has about 32 ribs,
the left with about 31, including in this count, the ribs forming
the edge of the dorsal margins; umbos wide, slightly depressed
or sulcated in the middle zone with the small beaks coiled a lit-
tle over the cardinal area; the beaks are placed at the anterior
one-third ; the shell is only moderately convex; in the left valve
the ribs are double in part over the anterior portion, simple else-
where, noded or beaded in the middle or umbonal section; on
older shells, the ribs of the left valve become narrow and _ sub-
triangular in section, heavier and stronger on the posterior sub-
margins; the ribs of the right valve are similar; interval be-
tween the ribs is etched with evenly to irregularly spaced lines ;
hinge straight with numerous small teeth arranged in two series,
nearly continuous, there being about 28 in the anterior set and
35 in the posterior; muscle scars well marked, the ventral mar-
gin fluted in harmony with the external ribs; cardinal area nar-
row with 3 chevron-shaped lines.

Length, 35 mm.; height, 18.5 mm.; semidiameter, 7.5 mm.
(right valve).

Compared with its most similar species, the Arca dariensis
Brown and Pilsbry of the Gatun Miocene and Arca concinna
Sowerby of the Recent fauna, this species differs by its more
transverse outlines, less convex, thinner shell and by its sculpture.
In Arca dariensis, the ribs on the posterior-umbonal slope are
double while in this species as in A. concinna, they are simple or
have only a faint, dividing line in the middle.

Type.—Paleontological Research Institution, No. 4082; other
specimens, No. 4083.

Occurrence.—Charco Azul.

30 BULLETIN 106 182

Genus NQGETIA (Gray) H. and A. Adams
Neetia reversa magma MacNeil
Netia magma MaeNeil, 1938, U. 8. Geol. Sur., Prof. Paper 189-A, p. 38,
pl. 6, figs. 20, 21.
Netia (Nwiia) reversa magma Pilsbry and Olsson, 1941, Proc. Acad. Nat.
Sci. Bhilas vol: 935 p- 90:

This large Netia is common as a Pliocene fossil along the
West Coast of northern Scuth America. One specimen, measur-
ing, length, 65 mm.; height, 61 mm.; and diameter, 32 mm., was
collected by Terry from the Pleistocene of Quebrada Rabo de
Puerco, When young, this subspecies cannot be readily separ-
ated from typical N. reversa except that in N. magma, the ribs
(counting the flutings along the inner margins) are generally
more numerous and the form tends to be longer or more regu-
larly rectangular. An imperfect specimen of V. magma from the
Pliocene of Rio Guanabanon measures length, 80 mm. ; height,
75 mm.-+ ; semidiameter, 4o mm. Our largest specimen of true
N. reversa, collected at Puerto Callo near Jipijapa, Ecuador, has
the following measurements, length, 51 mm.; height, 45 mm.;
semidiameter, 24 mm.

Occurrence.-—Pliocene. Rio La Vaca. Pleistocene. Rabo
des Perce:

Family PECTINID
Genus PSEUDAMUSIUM (Klein) Mérch
Pseudamusium terryi, n. sp. Plate’ 2; figs. 5. Gsm

Shell small, translucent, very thin, both valves only slightly
convex; beaks small, low, hardly projecting beyond the hinge
line ; ears small, subequal in the left valve; in the right valve, the
anterior ear is a little larger than the posterior and with a wide
fasciole corresponding to the byssal sulcus, above which are 6,
radial, scabrous threads separated by wide, unequal interspaces ;
on the right valve, the posterior ear is smooth, the anterior one
has a few to several, radial threads which fade out above; sculp-
ture of the right valve is variable, the umbonal portion is smooth,
below it, the surface is generally ornamented by widely spaced,
radial threads, numbering about 14 or very numerous, more
closely spaced threads numbering about 46; in addition, fine
but distinct “Camptonectes” striations are present; the right valve

183 Burics PENINSULA FOSSILS: OLSSON 31

is typically smoother with the radials numbering about 8, con-
fined to the anterior submargins in some valves, faint indications
of the radials may spread over the rest of the shell; the “Camp-
tonectes” striations are finer in the left valve but are visable with
a lens especially on the posterior submargins; interior with a
micalike lustre showing radially impressed lines corresponding
to the external sculpture.

Height,.15 mm.; diameter, 13.5 mm.; semidiameter, 1.25 mm.

This species resembles P. panamensis Dall® but differs by its
nearly smooth right valve. The shell is very thin and delicate.
It is locally common in the clays at Charco Azul.

Type.—Paleontological Research Institution, No, 4084; other
specimens, No. 4085.

Occurrence.—Charco Azul.

Family ANOMIIDZE
Genus PLACUNANOMIA Broderip

Placuanomia panamensis, n. sp. Plate i figs. 1, 4555
Shell of moderate size, thin to slightly thickened, Anomuia-like

in texture; lower valve widely adherent to the object to which
it was fixed; the upper valve concavely flattened to slightly con-
vex, sometimes developing an irregular fold along the margin;
the surface of the upper valve is smooth, sometimes with irreg-
ular, wormlike markings in some parts; under the lens, the
growth lines are seen to be irregularly arranged and wrinkled,
with very fine, scarcely visible, radial lines and near the margin
occasionally smali, appressed, spinelike scales can be noted; in
the lower valve, the surface is irregularly folded and shows fine
irregular, radial threads sometimes pustular, tubed and crowd-
ed, irregular growth lines; lower valve with a well-developed
v -shaped, crural process, fitting into deep sockets in the oppo-
site valve; the byssal foramin, large, filled with a plug, showing
externally as a long, wedge-shaped area extending to the beak:
and with a single muscle scar set obliquely below; in the upper
valve there are two muscle scars set obliquely to each other.

8 Dall, W. H.: The Albatross Report, Bull. Mus. Comp. Zool., vol.
43, No. 6, 1908, p. 404, pl. 6, figs. 8, 10. ‘

32 BULLETIN 106 184

Length, 60 mm.; width, 60 mm., upper valve.

Length, 53 mm.; width, 54 mm., upper valve.

Length, 34 mm.; width, 42 mm., lower valve.

From Placuanomia cumingii Broderip, the only other known
species along the West Coast, the fossil differs by its flat, feebly
plicated valves and in its more Anomia-like habitus of growth
and general sculpture. There are three valves in our collection,
the smallest being that of the lower or sessile valve. The crural
process is large and strong in the lower valve, fitting into corre-
sponding deep sockets in the upper valve.

Type.—Paleontological Research Institution, No, 4080; other
specimen, No. 4087.

Occurrence.—QOuebrada Rabo de Puerco.

Order ANOMALODESMACEA
Family PERIPLOMATIDZ
Genus PERIPLOMA Schumacher
Periploma lueina, n. sp. Plate 3, fig. 4

Shell of medium size, nearly circular in outline, the posterior
side somewhat shorter and narrower; the texture of the shell
is thin, formed by a pearly inner layer and an outer layer which
is paper thin and white or gray in color; both valves are of mod-
erate but nearly equal convexity with no noticeable flexing; the
surface markings consists mainly of fairly coarse, concentric
lines and very minute pustules or granules arranged concentric-
ally, strongest and crowded most on the posterior submargins ;
interior and hinge unknown.

Length, 38.5 mm.; height, 34.5 mm.; diameter, 17.5 mm.

We have two specimens but only the holotype is fairly well
preserved. In shape, the shell resembles a small Loripinus. The
granules are very small or submicroscopic in size and arranged
in a concentric series. |

Type.—Paleontological Research Institution, No. 5007.

Occurrence.—Rio Guanabanon.

Periploma planiuscula Sby. subsp.

Our collection has 2 large Periplomas from Rio Blanco which
measure respectively, 70 and 75 mm. in length. This is larger
than most Recent specimens of this species. They should per-
haps be separated as a subspecific form but the fossils are too
badly crushed for description and figuring.

Go

185 BurIcA PENINSULA FOSSILS: OLSSON

Periploma aff. stearnsii Dall

Periploma stearnsti Dall, 1896, Proc. U. S. Nat. Mus., vol. 18, p. 9.
Periploma stearnsii Dall, 1908, Bull. Mus. Comp. Zoél., vol. 43, No. 6, p.
426, pl. 16, fig. 5.

In form, the shell is subcircular to suborbicular with the beaks
placed at the posterior third; the texture is relatively thin with
an internal pearly layer, covered by a thin skin of a dull, white
color, The surface is thickly covered with minute or submicro-
scopic granules or pustules arranged in radial lines. The right
valve is a little more inflated than the left. Valves slightly flexed.

Length, 42 mm.; height, 37 mm.; diameter, 14 mm.

From the P. planiuscula group this species is distinguished by
its fine, radially arranged granules. In these characters, def-
inite affinities with P. stearnsiu Dall is indicated. Dall’s figure
of his species shows only the interior of a right valve which
makes a specific determination uncertain. Our only specimen
“js imperfect.

Occurrence.—Quebrada Penitas.

Order TELEODESMACEA
Family VESICOMYACIDA®

Genus CALYPTOGENA Dall
Calyptogena panamensis, n. sp. Plate 2, figs. 2, 3

Form elongate-ovate, moderately convex, thick-shelled, with
a coarse sculpture of crowded growth lines; anterior side about
\% the length of the posterior side with the low beaks curved for-
ward; anterior and posterior ends nearly equally rounded; no
lunule but apparently a long, narrow, excavated escutcheon is
present; texture of shell is solid; interior shows a deep, muscle
scar and a wide, simple pallial line; margin entire; teeth more
or less worn or obsolete in the only specimen showing the hinge
but with the remains of a large central and an anterior cardinal
present ; ligament external.

Length, 44 mm.; height, 24 mm.; semidiameter, 6 mm.

Calyptogena panamensis is the commonest and best preserved
fossil in the Burica sandstones. The shell is solid, generally some-
what chalky and the surface coarsely sculptured. The hinge ap-
pears to be that of typical Calyptogena but the teeth are worn or
imperfectly preserved in the few specimens showing the hinge.

34 BULLETIN 106 186

In a few specimens, the external ligament is still preserved. Per-
haps some of the species described as Plewrophopsis and Vest-
comya from the Oligocene of Peru may belong to Calyptogena
as suggested by Woodring but their hinge is not known while
their more Unio-like shape and flexed valves is more like
Pleurophopsis. The rock in which these fossils occur at Punta
3urica is a coarse, gritty or pebbly sandstone. They are associ-
ated with Solemya, Thyasira, Fissidentalium, Luciploma and
other forms. In a recent discussion of the depth range of Calyp-
togena pacifica Dall on the basis of the material preserved in the
National Museum, Woodring® notes that most of the examples
were dredged in quite deep waters ranging from 322 to 680
fathoms and a single corroded pair of valves from a depth
of 30 to 41 fathoms. Some of the specimens of Calypto-
gena from Burica Point occur as free valves but the majority
have closed valves, some still retaining remains of the external
ligament. Under these circumstances, it appears unlikely that
these shells could have drifted far from their original habitat
station.

Type.—Paleontological Research Institution, No. 4088; other
specimen, No. 4080.

Occurrence.—Punta Burica.

Family CONDYLOCARDIIDA

Genus CONDYLOCARDIA Bernard
Condylocardia panamensis, n. sp. Plates) ficsesQalo

Shell very small, generally glassy and solid in texture, equi-
valve and strongly inequilateral ; externally the valves are broad-
ly subtrigonal, the posterior side produced, pointed with a wide
excavated, escutcheonlike area which gives to the shell the ap-
pearance of a small Tridacna or a Verticordia; umbos prominent,
surmounted by the platelike, embryonic shell encircled by thick-
ened, raised margins; sculpture consists of strong, radial ribs,
heaviest in the middle, smaller on the sides and nearly absent
from the posterior extremity; these ribs on a typical shell num-
ber about 8; they are separated by rather wide interspaces, tra-

9 Woodring, W. P.: The Lower Pliocene mollusks and echinoids from

the Los Angeles Basin, California, U. 8. Geol. Sur., Prof. Paper 190, 1930,
Dp. ow.

or

187 Burica PENINSULA Fosstus: OLSSON

versely grooved or striated by the growth lines; hinge as normal
for the genus, in the right valve it has a strong knob or hook-
shaped anterior cardinal tooth and a socket for the left posterior
cardinal tooth, between which hes the ligamental pit, also a strong
anterior lateral tooth and a smaller, rudimentary posterior lateral
tooth; body cavity deep, the ventral margins fluted by the ends
of the ribs which usually show through the glassy or translucent
shell.

Length, 1.75 mm.; height, 1.50 mm.; diameter, 1.25 mm.

It is extremely interesting to discover a species of this genus
in the American fauna. Although at present known only as
fossil, it 1s doubtless present in the Recent Panamic fauna. The
headquarters of the genus Condylocardia’® lie in the southern
Pacific with several known species in New Zealand and Austra-
lia.1t One fossil species has been described from the Parisian
Eocene. The genus is characterized by its peculiar hinge and by
the persistant prodissoconch or embryonic shell which sits as a
small cap on the summit of the umbos. Our species differs striking-
ly from the known Recent species by its stronger ribs and deep,
excavated escutcheonlike area.

Type.—Paleontological Research Institution, No. 4090; other
specimens, No. 4091.

Occurrence.—Zone of unconformity at base of Pleistocene at

Punta Piedra.
Family THYASIRIDZ

Genus THYASIRA (Leach) Lamarck

Thyasira bisecta Conrad Plate 2, fig. 4

Venus bisecta Conrad, 1849, U. 8. Expl. Exped. (Wilkes), vol. 10, Geol.,
p. 724; Geol. Atlas, pl. 17, figs. 10, 10a.

Thyasira bisecta Dall, 1901, Proc. U. S. Nat. Mus., vol. 23, pp. 789, 790.

Thyasira bisecta Grant and Gale, 1931, Mem. San Diego Soc. Nat. Hist.,
vol: ll, pp: 281, 282, pl. 13) fig. 15. ;

For additional synonymy see Grant and Gale’s paper noted
above.

10 Bernard, F.: Jour. de Conch., vol. 44, 1897, p. 174.

11 For Australian species see, Cotton and Godfrey, Handbook of the
Molluses of South Australia, South Australian Branch British Science
Guild, 1938, pp. 191-196.

36 BuLLETIN 106 188

Our specimen is an internal cast composed of a pebbly sand-
stone matrix with small fragments of the original shell preserved
on the umbos and along the dorsal margins. The fossil measures,
length, 70 mm.; height, 70 mm.; semidiameter, 32 mm. It agrees
well with the figure of Thyasira bisecta Conrad, var. nipponica
Yabe as given by Grant and Gale of a specimen from the Plio-
cene of Japan. The geological range as given by those authors
extends from the Oligocene to the Pleistocene, its most southerly
known occurrence being in the Pleistocene of San Pedro. Its
Recent American range is given as off the Alaskan peninsula
south to the coast of Oregon. The occurrence of this species in
Panama is therefore of considerable interest. A large Thyasira was
described by VianWinkle from the Oligocene of Trinidad as T.
adocassa which appears to differ mainly in being somewhat more
elongated. Large Thyasiras are not uncommon in the Oligocene
of northern Colombia but have not been critically studied.

Figured specimen.—Paleontological Research Institution, No.
40092.

Occurrence.—Burica sandstones, Burica Point,

Family LUCINIDZE
Genus LUCINA Bruguiére
Subgenus LUCINOMA Dall
Lucina (Lucinoma) chiripanicia, n. sp. Plate 4, figs. 1, 4

Shell subquadrate to subcircular in form, only moderately con-
vex with a fairly thick texture; beaks small, pointed, recurved ;
dorsal area indicated by a depressed, ever widening zone, extend-
ing from the beaks to the posterior side, which is straight or
subtruncate ; the ventral side is widely rounded, the anterior side
a little produced, pointed, appearing slightly depressed; lunular
side, rather long; sculpture of fine growth lines and concentric,
sharp, distant, elevated lamelle continuous over the whole shell.
The elevated lamellz are spaced, 3.5 to 4 mm., apart on the
middle of the shell disk; the lunule is long, narrow, darker col-
ored than the rest of the shell; hinge of right valve shows two
strong, cardinal teeth, the posterior one being the heaviest and
bifid; anterior and posterior laterals visible but not strongly de-
veloped ; pallial line continuous ; the anterior adductor scar, long,
narrow.

189 BuricA PENINSULA FOSSILS: OLSSON 37

Measurements of the type, length, 54 mm.; height, 46 mm.;
semidiameter, 11.5 mm.

This species is nearest L. heroicus Dall from western Mexico
and to L. equizonatus Stearns from Santa Barbara channel,
California but differs from both by its form and in details of
sculpture. L. acutilineata Conrad (annulatus Reeve) has a more
circular, convex shell.

Type.—Paleontological Research Institution, No. 4099; other
specimens, No. 5000.

Occurrence.—Charco Azul.

Family VENERIDA
Genus PITAR Roemer
Subgenus LAMELLICONCHA Dall

Pitar (Lamelliconcha) mellisa, n. sp. Plate 5, fig. 4

Shell broadly subelliptical in form, ventral margin well round-
ed, posterior end more narrowly rounded; the shell is only mod-
erately convex, its surface ornamented with numerous, equal or
subequal, concentric ribs which are generally thin or lamellose
and separated by somewhat wider, flat interspaces; there is a
tendency for each 4th or 5th concentric rib to become enlarged
or lamellose and the interspaces, as well as the ribs, are covered
with fine, submicroscopic striz; escutcheon very narrow ; inter-
ior concealed in our specimen.

Length, 47 mm.; height, 40 mm.; semidiameter, 12 mm.

The holotype, from Quebrada Mellisa, is the only specimen
known. It differs most strikingly from the members of the
Pitar circinata group by its more regularly elliptical form and
wider, more rounded posterior side.

Type.—Paleontological Research Institution, No. 40095.

Occurrence.—Quebrada Mellisa.

Pitar (Lamelliconcha) anona, n. sp. Plate 5, fig. 1

Shell subovate, plump, ventral margin regularly rounded; pos-
terior side narrowed with a tendency to become obliquely trun-
cated at its end; surface ornamented with prominent, subequal,
concentric ribs which are thin or lamellar and separated by deeper
and wider interspaces; these ribs are thin and high but they are

38 BULLETIN 106 190

generally not well preserved over the whole surface; finer con-
centric striz overrun the concentric ribs and their interspaces ;
lunule small, cordate, marked with lower ribs; escutcheon nar-
row, tidgelike ; interior is concealed in our specimen.

Length, 35.5 mm.; height, 28.5 mm.; diameter, 20 mm.

Known only from the holotype which is a perfect shell with
closed valves and consequently the interior cannot be seen, From
P. circinata the species differs in being longer and by its more
strongly truncated posterior side as well as by its thinner and
higher riblets. A weak sinal depression extends from the pos-
terior-ventral side towards the umbos.

7 ype.—Paleontological Research Institution, No. 4096.

Occurrence.—Rio Guanabanon.

Genus MACROCALLISTA Meek

Macrocallista traftoni, n. sp. Plate 5, figs. 2, 3

Shell medium-sized, subelliptical in form and moderately con-
vex; texture subsolid, porcellaneous with a smooth external sur-
face which is generally polished but originally was covered with
a brownish-colored epidermis of which remnants persist on some
specimens ; the posterior side is twice the length of the anterior,
oblique and obtusely rounded at its end; muscle scars prominent,
united by the pallial line with a wide sinus reaching past the
middle line; hinge normal; lunule narrow, slightly impressed.

Length, 33 mm.; height; 21 mm.; semidiameter, (Gs) em:
(type. )

Length, 39.5 mm.; height, 28.5 mm.; semidiameter, 8.75 mm.

Although common, it has not been possible to identify this
fossil with any known species. From the young of the Recent
West Coast species of Macrocallista, such as M. aurantiaca Sby.,
M. squalida Sby., and M. pannosa Sby., the present shell differs
by its longer form. Some shells have remains of a brown epi-
dermis but show no trace of a color pattern,

Type.—Paleontological Research Institution, No. 4093; other
specimen, No. 4094.

Oceurrence.—Pleistocene, Rabo de Puerco and Rio Guanaba-

191 Burica PENINSULA FossILs: OLSSON 39

non.

Genus LUCIPLOMA, new genus

Genotype—Luciploma panamensis, n. sp.

The following is a description of the genus Luciploma.

Shell subovate, longer than high, solid and with an external
concentric sculpture ; no lunule or escutcheon ; hinge venerid with
a set of 3 cardinal teeth but no laterals; resilium scar very high
and wide, not bordered above by a groove for the insertion of the
external ligament; dorsal edge of the valve sharp, flangelike ;
nymphs if present much reduced in size; ventral margins smooth.

Remarks.—The type of this interesting genus is a fragmen-
tary right valve. Its hinge structure agrees best with Cyclina and
Cyclinella, the right valve having no anterior lateral and 3 typical
venerid cardinal teeth of which the middle one is strongest. Both
Dosinia and Cyclina have broad nymphs and the resilium scar
is bordered dorsally by a deep groove for the insertion of the ex-
ternal ligament. In the type of this new genus, the nymphs are
not recognizable, the whole area above the cardinal teeth form-
ing the resilium scar. There is no dorsal ligament groove as in
Dosima, the external edge of the shell forming a sharp, flangelike
margin. The anterior muscle scar is deep as in all thick, solid
shells. The ventral margin is smooth. Lunule and escutcheon
are absent.

Luciploma panamensis, n. sp. Platemssetesealene

Shell subovate, solid and of medium convexity; external
sculpture formed by concentric riblets which are quite regularly
spaced on the umbo but become crowded and irregular ventrally ;
inner margins smooth; hinge as described above, the most strik-
ing feature being the high, wide resilium scar which forms a
sharp, flangelike edge to the dorsal margin of the shell: anterior
muscle scar prominent.

Partial length, 38 mm. ; height, 36 mm.; semidiameter, 11 mm.

Although it has been necessary to base a new genus and spe-
cies on a single, fragmentary specimen, its characteristics are so
unusual that its naming appears justifiable. The hinge structure
as indicated above is typical venerid, the relations of the shell be-
ing clearly with Dosinia and Cyclina, It differs principally from
these and other venerid genera by its wide resilium scar. The

40 BULLETIN 106 192

external sculpture is suggestive of certain species of Astarte and
Crassatellites.
T ype.—Paleontological Research Institution, No. 5000.

Occurrence.—Burica sandstones, Burica Point.

Genus CHIONE Megerle von Mihlfeld
Subgenus CHIONE, s. s.

Chione (Chione) vaca, n. sp. Plate 5, fig. 7

Shell of medium size, subtrigonal, very solid, depressed to
strongly convex; the form is subtrigonal ; the umbos surmounted
by the slightly recurved beaks, are placed a little in front of the
middle, and the posterior and anterior sides are straight, sloping
and of nearly equal length; ventral side evenly rounded; sculp-
ture is formed of strong, steplike, concentric folds, widening ven-
trally, and strong, radial riblets or cords which tend to be regu-
lar near the ventral margins but which dorsally are paired or
formed by the division of earlier simple cords; escutcheon and
lunule well marked, without ribs; hinge normal with a strong,
central cardinal tooth; ventral margin crenulated.

Length, 27.5 mm.; height, 26 mm.; semidiameter, 8.75 mm.

Length, 28 mm.; height, 30.5 mm.; semidiameter, 12 mm.

Allied to the Recent West Coast, C. subimbricata Sby., this
species is readily distinguished by its peculiar step or platform-
like ribs and trigonal form. In the young of C. subimbricata, the
concentric ribs have raised, thin edges so that the shell resembles
C. cancellata. This stage, if present in C. vaca, must be restricted
to a very early age as the shoulders of the ribs are rounded even
in very small shells.

Type.—Paleontological Research Institution, No. 4097.

Occurrence.—Rio La Vaca. (Quebrada Melissa.
Chione (Chione) araneosa, n. sp. Plate 3, fig. 6

The shell is of medium size, solid, obliquely subtrigonal and
of medium convexity; posterior-dorsal side appears nearly
straight with the edge, bordering the excavated, flattened escutch-
eon, angled; ventral side well rounded; the surface sculpture is
rather subdued and is formed principally by radial cords crossed
iby weak concentric ridges; the radial cords are rather coarse
and regular over major part of the surface and appear slightly
curved as they cross from the beaks to the ventral margin; on

193 BuricA PENINSULA FossIus: OLSSON 41

the dorsal-posterior slope, the radials are much finer; the con-
centric ridges are subobsolete for the most part and are well
marked only on the umbos; on perfect specimens, they were
probably lamellose to a degree on the posterior-dorsal submar-
gins, particularly near the end; lunule subelliptical, defined by
an impressed line; interior not exposed.

Height, 32 mm.; length, 33 mm.; semidiameter, 7 mm.

The species resembles an eroded Chione cancellata but the
shell is higher, more trigonal, solid and the primary radials are
simple cords.

Type.—Paleontological Research [nstitution, No. 4008.

Occurrence.—Burica sandstones, Burica Point.

Subgenus LIROPHORA Conrad
Chione (Lirophora) kelletti (Hinds)
Venue kellettit Hinds, 1844, Zool. Voy. Sulphur, Moll., p. 65, pl. 19, fig. 5.
Chione (Lirophora) kelletti Pilsbry and Olsson, 1941, Proe. Acad. Nat.
Sei. Phila., vol. 93, p. 64, pl. 16, fig. 2.

This species was described by Hinds from the island of Quibio,
off the coast of the Province of Veragua, Panama. It is appar-
ently a rare species in the Recent fauna. As fossil, it is common
at several localities on the Burica Peninsula. It is quite variable,
some individuals being much longer than high, while in others,
the height is nearly the same as the length. The solid coalescent
ribs tend to form a smooth, even surface on the middle of the
disk with a bordering band of high, leaflike expansions on the
ends, often broken away. These thick, solid shells resemble spe-
cies of Anomalocardia but differ in possessing the foliaceous
areas on the anterior and posterior sides. The pallial sinus is
very short. Some of our specimens measure as follows.:

Length, 48.5 mm. ; height, 40.0 mm. ; diameter, 15.0 mm.

Length, 42.5 mm.; height, 38.0 mm. ; diameter, 27.5 mm.

Length, 34.0 mm.; height, 27.5 mm. ; diameter, 9.0 mm.

Occurrence.—Rio La Vaca. Quebrada Mellisa.

Chione (Lirophora) ebergenyi Bése

Venus (Chione) Ebergenyii Bose, 1906, Bol. Inst. Geol. Mexico, Num.
22, lam. II, figs. 4-17.

A specimen of Lirophora from Quebrada Mellisa is evidently
the Chione ebergenyi Bose from Paso Real near Tuxtepec, State

49 BULLETIN 106 ; 194

of Oaxaca in Mexico. The shells figured by Bose are slightly
longer and the coste are narrower and hence more numerous.
Most species of Lirophora are variable and consequently these
differences are not considered of much importance.
Occurrence.—Quebrada Mellisa.
Family PSAMMOBIIDE
Genus SANGUINOLARIA Lamarck

Subgenus SANGUINOLARIA, s. s.
Sanguinolaria (Sanguinolaria) azulensis, n. sp. Plate 5, fig. 8

Shell small, subelliptical, thin and slightly convex; the umbos
are nearly central ending above in the small, pointed beaks ; pos-
terior side slightly narrower than the anterior, its dorsal margins
somewhat flattened and smooth, there being no well-marked pos-
terior flexure; sculpture is formed by evenly spaced, concentric
lines, strongly developed on the anterior side, nearly absent from
the posterior, while in the middle zone they are slightly oblique
and cross the concentric growth lines; no radials; interior fea-
tureless, the pallial sinus and muscle scars scarsely showing be-
cause of the thinness of the shell; hinge of the right valve with
2 cardinal teeth, the posterior one being double, 2 laterals, the
anterior one placed near the cardinals, the other one more re-
mote.

Length, 35.5 mm.; height, 21 mm.; semidiameter, 4.25 mm.

Our material of this interesting form consists of two speci-
mens, one badly broken. From the Recent West Coast, S. telli-
nides C. B. Adams, it is distinguished by its smaller, thinner
shell and absence of any radial sculpture.

Type.—Paleontological Research Institution, No. 5008.

Occurrence.—Pliocene. Charco Azul.

Family TELLINIDZA Linné
Genus TELLINA Linné

Subgenus MACALIOPSIS Cossmann

Tellina (Macaliopsis) frontera, n. sp. Plate 4, figs. 3, 6
Shell suborbicular, Semele-like in form: the valves are mod-
erately convex, that of the left being a little more inflated than
the right which has a shallow flexure extending across the pos-

terior-middle section; beaks placed a little posterior of the mid-

195 BuricA PENINSULA FOSSILS: OLSSON 43

dle are small, adjacent and project but little above the hinge line;
anterior side, nearly twice the length of the posterior, is widely
rounded at the end, its dorsal margin sloping downward; pos-
terior-dorsal side sloping more rapidly than the anterior, joining
with the ventral side to form a well-rounded end; ventral margin
straight in the middle, oblique to the longer axis of the shell,
rounding into the side; the valves are weakly flexed, resulting in
the formation of a shallow, broad, depressed zone in the posterior-
middle section of the right valve; there is a narrow, linear, pos-
terior-dorsal area in each valve; surface sculptured by moder-
ately coarse and evenly spaced growth lines; interior unknown.

Length, 44 mm.; height, 36.5 mm.; diameter, 15 mm.

In the holotype the two valves are tightly closed so that the
interior and the hinge are not visible. The shape and sculpture
are quite Semele-like but the presence of a well-marked posterior-
dorsal area and the distinct but slight flexing of the valves indi-
cate tellinid rather than semelid affinities.

Type.—Paleontological Research Institution, No. 5001.

Occurrence.—Quebrada Penitas. Costa Rica.

Genus MACOMA Leach

Subgenus PANACOMA, new subgenus
Genotype—Macoma (Panacoma) chiriquiensis, n. sp.

The following is a description of the subgenus Panacoma.

Valves thin, broadly subovate, moderately inflated and sub-
equal; the posterior side a little narrower and longer than the an-
terior; sculpture of strong, raised, concentric threads and a
sprinkling of small, Thracia-like granules; no differentiated pos-
terior flexure; hinge normal; pallial sinus wide, confluent below.
Macoma (Panacoma) chiriquiensis, n. sp. Rieter beaticse 516

Shell thin, broadly subovate, subequal; the anterior side is
somewhat shorter and more widely rounded than the posterior ;
there is no posterior flexure so that the two sides appear more
or less subequal; the sculpture is formed by fairly regular, small,
raised threads which are weakly flexed in the middle by a slightly
depressed band extending from the beaks to the middle portion
of the ventral side; in addition, the surface has a sprinkling of
small granules recalling some species of Thracia; body cavity
deep with a wide pallial sinus reaching a little beyond the middle,

-

44 BULLETIN 106 196

below, it is confluent with the pallial line which reaches nearly
to the posterior muscle scar; hinge of the left valve with normal
Macoma-tooth formula, 2 cardinal teeth, the anterior one larger,
no laterals.

Length, 34 mm.; height, 27 mm.; (estimated) semidiameter, ~
7 nin. Lye).

This species is based on two imperfect specimens but with
very distinctive characters. The valves are moderately inflated,
thin with no posterior flexure. The surface sculpture is peculiar
and consists of a series of strong, concentric, raised threads sep-
arated by wide, flat interspaces, the whole being covered with
small granules sometimes fusing with the coarse threads of
growth.

Type.—Paleontological Research Institution, No. 5002; other
specimen, No, 5003.

Occurrence.—Charco Azul.

Subgenus MACOPLOMA Pilsbry and Olsson

Macoma (Macoploma) medioamericana, n. sp. Plate 4, fig. 8

Shell of medium or large size, elongate, delicate; the valves
are subequal, the left being slightly larger and more convex than
the right which is somewhat flexed or depressed in the middle;
beaks, placed at the posterior one-third, are small and pointed;
anterior side nearly twice the length of the posterior, obliquely
rounded at the end; posterior side somewhat narrowed, obliquely
truncated at the end; surface is marked with lines of growth,
smoother in the middle, coarse and more or less granulose on
the sides ; each valve has a narrow, submarginal zone at the pos-
terior end, its surface earthy in appearance and bordered anterior-
ly by a line of coarse granules; hinge unknown.

Length, 62 mm.; height, 30 mm.; diameter, 12 mm.

Length, 52 mm. (imperfect) ; height, 27 mm.; diameter, 12 mm.

The type of this subgenus is Macoma ecuadoriana Pilsbry and
Olsson, recently described from the Pliocene of Ecuador. The
Panama species is proportionately longer. It differs also by its
coarser, more earthy, or Thracia-like granulation of the surface
on the posterior submargins. Although common at Quebrada
Penitas, the species is seldom well preserved. Fragments indi-
cate that the shell in some cases reached 80 to 85 millimeters in

197 BuricaA PENINSULA FossILs: OLSSON 45

length.
Type.—Valeontological Research Institution, No. 5004.
Occurrence.—Pliocene. Quebrada Penitas, Costa Rica.
Family CORBULIDZ
Genus CORBULA Bruguiere
Subgenus VARICORBULA Grant and Gale
Corbula (Varicorbula) granti, n. sp. Plate 2, figs. 8, 9

Shell of medium size, subtrigonal, moderately convex and with
nearly central beaks ; valves unequal, that of the right being about
a fourth larger, both are quite convex; right valve is bluntly ros-
trate posteriorly, and its surface sculptured with strong, concen-
tric riblets which pass into crowded irregular lines on the pos-
terior area; left valve smaller, its posterior half more or less im-
pressed, its anterior side rounded to convex and its surface marked
with subobsolete to irregular, smoothish concentric riblets, no
radial lines; the left valve is rostrated, its posterior area marked
with 3, low riblike folds, most distinct at the ends; interior of
valve deep, the right valve with a strong cardinal tooth, fitting
into a socket in the left.

Length, 11.5 mm.; height, 10 mm.; semidiameter, 4.5 mm.
(right).

Length, 10.5 mm.; height, 9 mm.; semidiameter, 4 mm. (left).

Our specimens are all rather poorly preserved, some of the
valves being deeply weathered and chalky. From the majority
of Corbulas of this group, the present species differs in the ab-
sence of radial lines on its left valve. Both valves are moder-
ately convex and marked with concentric riblets, those of the
right valve being stronger

Type.—Paleontological Research Institution, No. 5005; other
specimen, No. 5006.

Occurrence.—Quebrada Penitas. Charco Azul.

Corbula (Varicorbula) cf. bradleyi Nelson
Corbula bradleyi Nelson, 1870, Trans. Conn. Acad. Sei., vol. 2, p. 200.
Corbula (Aloidis) bradleyi Spieker, 1922, Johns Hopkins Univ., Studies
Geol. No. 3, p. 171, pl. 10, figs. 13, 14.

Corbula (- - - -) bradleyi Olsson, 1932, Bull. Amer. Paleont., vol.
II fo, Weir

Shell large, the right valve larger and more convex than the

left; umbos wide, convex, with the beaks near the anterior one-

46 BULLETIN 106 198

third, incurved over the hinge, the posterior side bluntly rostrate
and marked off from the rest of the surface by a weak ridge; the
surface sculpture of the right valve consists of strong and nearly
regular, concentric riblets; the left valve is smaller and more
elongated in form and less convex; its surface sculpture is formed
by irregularly spaced, narrow, radial riblets.

Nelson described this species from a single, somewhat weath-
ered right valve from the Tumbez beds of northern Peru. The
type was subsequently studied and figured by Spieker. This
specimen measures length, 20 mm., and height, 18.5 mm., a size
rather large for the genus.

A Varicorbula probably belonging to Nelson’s species occurs
in our collections from Quebrada Mellisa. We have 5 right
valves and 1 left valve. Two valves have the following measure-
ments: right valve, length, 16 mm.; height, 12.5 mm.; semi-
diameter, 6.5 tmm.; left valve, length, 11 mm.; height, 8 mm.;
semidiameter, 4 mm.

A relatively large Varicorbula from the Pliocene of California
has been described as Il’. gibbiformis by Grant and Gale.’* The
figures seem to indicate a higher form than the Panamanian spe-
cimens.

Class GASTROPODA
Order CTENOBRANCHIATA
Family TEREBRIDZ
Genus TEREBRA Bruguiere

Subgenus STRIOTEREBRUM Sacco
Terebra (Strioterebrum) guanahana, n. sp. Plate 11, fig. 4

Shell large, slender with about 12 whorls preserved in the type
(apex missing); the sculpture of the earlier whorls is rather
strong with a prominent fasciolar band defined below by a deep
spiral groove which appears punctate in the spaces between the
ribs ; on the lateral whorls, the fasciolar band becomes wider and
the limiting groove below it is less strong; the spirals overrun
the whole surface including the fasciolar band, at first strong and
regular on the spire whorls they soon become more numerous
and irregular on the later turns; on the whorl of the spire about

12 Grant, U. S. IV, and Gale, H. R., San Diego Soe. Nat. His!., Mem.,

vol. I, pp. 420-421, pl. 19, figs. 4-6. Also Woodring, 1938, U. S. Geol. Surv.,
Prof, Paper 190, 1931, p. 55, pl. 6, figs. 8, 9.

199 BuricaA PENINSULA Fossius: OLSSON 47

12 mm. from the tip, the ribs are strong, slightly bowed and
number about 23 with about 6 or 7 spirals in their interspaces ;
on the succeeding turns, the ribs gradually become more numer-
ous and less pronounced, and on the last turn appear scarsely
stronger than crowded growth lines; the spirals on the mature
whorls numerous, irregular and rather weak; anterior canal
fairly long, twisted, the columella armed with 2 low folds.
Length, 69.00 mm. ; diameter, 14.25 mm. (type).
Type.—Paleontological Research Institution, No. 4026.
Occurrence.—Rio Guanabanon, Sta. 18.
Terebra (Strioterebrum) aspera Hinds
Several poorly preserved Terebra in our collections have been
tentatively identified with this Recent species. They are quite
similar to specimens of 7. aspera from the West Coast of South
America but differ in a few minor characters, the constancy of
which cannot be determined from the material at hand.
Occurrence.—Rio La Vaca and Rio Guanabanon.

Terebra (Strioterebrum) cracilenta Li Plate 11, fig. 5
Terebra cractlenta Li, 1930, Bull. Geol. Soc. China, vol. 9, No. 3, p. 274,
pl. 8, fig. 67.

Terebra cracilenta Pilsbry, 1931, Proe. Acad. Nat. Sci. Phila., vol. 83,
pp. 434, 439, text figs. 1, la, 2.

Terebra (Strioterebrum) cracilenta Pilsbry and Olsson, 1941, Proce. Acad.
Nat. Sci. Phila., vol. 93, p. 14.

Of this beautiful species, we have 3 specimens, none quite per-
fect. The columellar folds are weak and sometimes scarsely de-
veloped, the superior one being generally broad and _ flattened.
The spiral sculpture predominates and consists typically of alter-
nating bands nodulated by the ribs, this noding extending to
the spiral bands on the base.

Specimen figured.—Paleontological Research Institution, No.
4027.

Occurrence.—Rio La Vaca.

Terebra (Strioterebrum) vaca, n. sp. Plate 11, figs. 6,:7

Shell acute-acuminate, the taper being rather rapid; whorls
about 10 or more (apex lost on type) straight with the fasciolar
band projecting slightly above the general surface; each spire
whorl is rather wide with noticeably inclined sutures; the su-

48 BULLETIN 106 200

tural fasciole is pronounced and strongly noded, especially on
the upper half, there being on the last turn about 24 nodes pres-
ent; below the sutural fasciole, the face of the whorl has 4 spiral
bands with a 5th just visible in the lower suture on some whorls,
these spirals increase in strength upward; the ribs are weak and
mainly indicated by the noding of the spirals and in the spiral
interspaces are scarsely shown; on the outer face of the last
whorl, there are altogether about 13 spirals, the lower 4 or 5
encircling the base, are slightly smaller and plain; anterior canal
twisted, the columella with 2 strong folds, the upper one contin-
uous with the sharp, external keel.

Length, 42.00 mm.; diameter, 10.50 mm.

Type.—Paleontological Research Institution, No. 4028.

Occurrence.—Rio La Vaca. |

Terebra (Strioterebrum) panamillata, n. sp. Plate 11, fig. 3

Shell of moderate size with about 7144 whorls preserved in the
type (apex missing) ; fasciolar band is strongly noded and about
one-third of the width of each spire whorl; it projects slightly
above the general surface, otherwise the surface profile is near-
ly straight ; although the ornamentation consists of both ribs and
spirals, the sculpture as a whole appears smoothish; the spirals
cover the entire surface, including the fasciole and are mainly
flat bands somewhat stronger in the middle of the whorl but de-
crease in strength on the base; in the interval below the sutural
fasciole and the suture, the spiral sculpture falls into two series,
a lower set formed by 4 flattened bands, quite regular and an
upper set of lower, narrower and more irregular ones; the ribs
are weaker than the spirals except on the fasciole which they
strongly nodulate; on the last whorl, the ribs are narrow, sinu-
ous, widely spaced and number about 12 but they do extend
over the base; the twisted anterior canal rather short and the
columella folds are weakly developed, only the superior one be-
ing at all recognizable.

Length, 32 mm.; diameter, 9 mm.

This species resembles 7. armillata Hinds of the Recent fauna
as well as its subspecies sheppardi Pilsbry and Olsson from the
Ecuadorian Pliocene but differs in its smoother sculpture, weaker

POL Burica PENINSULA Fossius: OLSSON 49

columellar folds and other characters. It also resembles 7.
ligyrus Pilsbry and Lowe but is larger and the fasciolar groove
is more strongly defined.
Type.—Paleontological Research Institution, No. 4020.
Occurrence.—Rabo de Puerco.

Family CONIDA
Genus CONUS Linné
Subgenus LEPTOCONUS Swainson
Conus (Leptoconus) arcuatus vacuanus, n. subsp. Plate 6, figs: 11, 12

Shell of medium size with a sharply angled shoulder and
broadly conic, high spire; the nucleus was very small but is lost
on all our specimens, it was followed by 10 or more spire whorls,
the earliest of which are ornamented by small ribs which are
quickly lost on the succeeding turns; the surface of the spire
whorls is concave or excavated, leaving the edge of the shoulder
sharply angular; the last whorl is rather wide at the shoulder,
tapering rapidly forward into the anterior canal which is slightly
twisted at the end; the sculpture, in the young stages, consists
of strong, spiral grooves which cover the whole surface except
the spire and possibly a narrow band adjacent to the shoulder ;
these spiral bands are separated by strong grooves and generally
average about 22 in number; these bands may be regular in size
and width or they may be divided by medial lines; in older
shells, a wide zone bordering the shoulder may be smooth or it
may have only faint indications of the spiral bands remaining
visible; columella straight, the anterior canal with a slight twist
or fold at its end.

Length, 46 mm.; height, 22 mm. (type).

Length, 36 mm.; height, 18 mm.

This cone recalls some Miocene species as C. planiliratus Sby.
and C. imitator liws Woodring.** Like other members of this
group, the cone shows much variation in sculpture according to
age and size. Amongst Recent forms, the present shell is closely
allied to Conus arcuatus* Sowerby. Conus gradatus, as figured
by Reeve,’ is possibly the same as Sowerby’s species. In the

13 Woodring, W. P.: Miocene mollusks from Bowden, Jamaica, Car-
negie Inst. Washington, Pub. No. 385, 1928, p. 209, pl. 10, figs. 5, 6.

14 Sowerby, G. B.: The Conchological Ilustrations, Conus, 1841, fig. 9.
15 Reeve, L.: Conchologia Iconica, 1843, fig. 140.

50 BULLETIN 106 202

series before me, the fossil differs by its wider form and shorter,
more evenly conic spire, the tip of which is scarcely attenuated.
A cone from the Pleistocene of the Rio Guanabanon identified as
C. arcuatus is figured for comparison. ‘This shell is immature
but is very similar to the form figured by Reeve as C. gradatus.
G@Plate(G, fess.)

Type.—Paleontological Research Institution, No. 4030.

Occurrence.—Quebrada Pefiitas, Quebrada Mellisa and Rio
Guanabanon. .

Family TURRIDZE
Genus POLYSTIRA Woodring

Polystira panamensis, n. sp. Plate 12, fig. 4

Shell of medium size, fusoid, the aperture and spire of about
equal length; nucleus unknown, about 8 whorls remaining on
the type specimen; the spire whorls have a strong, spiral cord
placed a little below the middle and sculptured with double-
knobbed ribs, which lie at the apex of the anal sinus; above and
below this central or peripheral cord, the growth lines curve
forward as strong, raised threads; the upper suture is bordered
by a raised thread and in the area between it and the central
cord, the surface has 4, small but well-marked, spiral threads
but no primaries; the last whorl has 5 primary spirals between
the peripheral cord and the base, these are more widely spaced
above, their interspaces carrying 2 or more fine threads; below
the base, there are 10 or mote spirals which extend over the
anterior canal; aperture wide above, narrowed forward; axis
of anal sinus in the middle following the peripheral cord.

Length, 23 mm.; height, 8 mm.

A single specimen only of this finely sculptured species was
found.

Type.—Paleontological Research Institution, No. 4032,

Occurrence.—Charco Azul.

Genus CLATHRODRILLIA Dall
Clathrodrillia harrisi, n. sp. Plate 9, fig. 10; Plate 11, fig. 8

Shell of medium size, slender, the spire half again as long as
the aperture; apex acute, originally with a very small nucleus
(lost on our specimens) ; the subsequent whorls number about

203 Burica PENINSULA Fossits: OLSSON 51

10, are convex in profile and separated by distinct but somewhat
wavy, appressed sutures; sculpture, formed by spirals and ribs,
is rather weak and subdued; the short ribs are restricted to the
middle of the whorl (absent from the concave sutural fasciole
and the base) ; these ribs on the last whorl number about 14;
spiral threads have a variable development, on some specimens
as illustrated by figure 8, Plate 2, they are quite strong and cover
the ribs, in others they are nearly absent from the top of the
ribs and are strongly developed on the base only; very fine
spiral threads cover the entire surface and may be seen with a
hand lens; aperture subovate, terminating forward in a rather
wide, slightly recurved canal; outer lip thickened by a humped
rib on the back and with a small, narrow anal sinus lying
in the sutural fasciole ; columella with a spread of callus.

Length, 34 mm.; diameter, 11.75 mm.

Length, 32.5 mm.; diameter, 11 mm.

This species is referred tentatively to Clathrodrillia, In form
and thickened lip it recalls Glyphostoma or Clathurella but dif-
fers in other characters.

Type.—Paleontological Research Institution, No. 4033.

Occurrence.—Quebrada Penitas.

Subgenus BURIDRILLIA, new subgenus

Genotype.—Clathrodrillia panarica, un. sp.

The following is a description of the subgenus Buridrillia.

The shell is rather large, slender, fusiform with a long spire
and anterior canal; anal sinus like that of Drillia is placed in an
excavated fasciolar band bounding the upper suture; pillar
straight, generally with a large, thick fold on the columella; an-
terior canal long, wide, nearly straight; sculpture of straight
axial ribs and spirals, the surface with a waxy lustre.

To this group, we should probably also refer the Borsonia
ephigona Von Martins'® described from deep-water stations in;
the Indian Ocean and from off the coast of Sumatra (depths
614 to 677 meters in depth). The type of the Indian Ocean spe-

16 Von Martens, Ed., und Thiele, J.: Die beschalten Gastropoden der

deutschen Tiefsee Expedition, 1898-99, Wissen. Erg. Deutsch. Tiefsee Exp.
Dampfer ‘‘ Valdivia,’’ Band, 1904, p. 91, taf. 2, fig. 2.

iy) BULLETIN 106 204

cies is very similar in form and sculpture and the columella has
a large, thick fold. The known specimens are small (the largest
measuring but 28 millimeters) and may not be mature but the
columellar fold is large and in an advanced stage of development.
The genus Darby, recently proposed by Bartsch’ for D. lira of
the Puerto Rican deep, has a similarly large, thickened columellar
fold but differs in other respects.
Clathrodrillia (Buridrillia) panarica, n. sp. Plate’ 7, figs. .4.s5ece

Shell quite large, fusiform, rather coarse and solid; whorls
8 or more; nucleus not known; sculpture consists (a) of narrow,
foldlike ribs which are strongest on the spire whorls where they
extend from the lower suture to the edge of the anal fasciole but
on the last whorl are mainly restricted to the portion immediate-
ly adjoining the fasciole, and (b) faint, subobsolete spirals ; on the
holotype, the ribs number 12 or 13 on the last turn; the spirals
are flattened, smoothish or irregular cords, a little coarser on
the anterior canal, absent from the surface of the fasciole; the
spirals number about & on the penulimate whorl and about 30
on the last whorl; outer lip sinuous, curved forward in the lower
portion and with a moderately deep sinus lying in the anal
fasciole; aperture elongate, ending in a fairly wide, anterior
canal; columella with a large, thick, lumplike fold, its upper or
posterior side, flattened or excavated.

Length, 72.0 mm.; diameter, 20.5 mm.; aperture, 31.0 mm.

This peculiar species is characterized by its large size, waxy
surface luster, and especially by the large columellar fold. This
fold is not equally developed on all shells and its size is probably
not entirely a result of mature growth. Some specimens from
Quebrada Penitas, as large as the average shell from Charco
Azul, may have a plain columella or one showing only a slight
swelling while other shells from the exposures along the beach
on the west side of the Burica Peninsula have developed a large,
thick fold at the same stage of growth. The axial sculpture is
formed by strong, narrow, ribs which commence on the base and
extend to the edge of the sutural fasciole. The spirals form sub-
obsolete, flattened bands separated by fine lines.

17 Bartsch, P.: New mollusks of the family Turritide, Smith. Mise. Coll.,
vol. 91, No. 2, 1934, p. 22, pl. 6, figs. 4, 5; pls i Higs, Go7s.

205 BuricaA PENINSULA FoOssIus: OLSSON 53

Type.—Paleontological Research Institution, No. 4034; other
specimens, No. 4035.

Occurrence.—Quebrada Penitas, Costa Rica; Charco Azul,
Panama. Beach exposures on the west side of the Burica Penin-
sula, Costa Rica.

Genus ANCISTROSYRINX Dall

Ancistrosyrinx cedonulli reevei, n. subsp. Plate 10, fig. 4
ef. Plewrotoma cedonulli Reeve, 1843, Proce. Zool. Soc. London, p. 185.
ef. Pleuwrotoma cedonulli Reeve, 1845, Conch. Icon. Pleurotoma, sp.

IEG
ef. Ancistrosyring cedonulli Dall, 1908, Albatross Report, p. 273.

Shell broadly fusiform, with a high, tabulated spire, elegantly
coronated with a row or crown of triangular, flattened, scalelike
spines; surface generally smoothish and polished, in places mal-
leated or showing a series of wrinklelike, spirally arranged threads
and a set of strong spirals on the anterior canal; in the area be-
tween the shoulder and the suture, the surface is flattened with
a strong central carina and sculptured with a series of oblique
growth lines on the outer portion, smoother on the inner side;
anal sinus deep, lying next to the suture; the scalelike spines
decorating the shoulder, number about 19 on the last whorl.

Length, 43 mm.; diameter, 20 mm ; aperture, 27 mm.

The type of Pleurotoma cedonulli was dredged by Cummings
in the Bay of Panama at a depth of 10 fathoms. It is an imma-
ture specimen. KReeve’s figure shows a narrow, slender shell
with relatively few spines on the shoulder angle. Our fossil
specimens are wider and have more shoulder spines. The fossil
is quite common at Charco Azul, the delicate shell having a
high surface polish and a white to cream color.

Type.—Paleontological Research Institution, No. 4036.

Occurrence.—Charco Azul. Rio Guanabanon.

Genus FUSITURRICULA Woodring
Fusiturricula woodringi, n. sp. Plates ieencoe2
Shell quite large, slender, fusiform; spire and anterior canal
very long and of equal length; nucleus not preserved, subsequent
whorls 10 or more in number; sutures indistinct, appressed, in

$4 BuLLETIN 106 206

front of which the whorl is deeply constricted to form a_ pro-
nounced sutural fasciole; on the last whorl, the sculpture has 10,
short, axial ribs developed principally on the shoulder with the
last rib forming the back of the lip being the largest and strong-
est; in addition there are spiral threads arranged in an alternat-
ing series of primary, secondary and tertiary size and extend
from the tip of the anterior canal to the sutural fasciole; on the
fasciole itself, the spirals are much finer; aperture subovate, with
a long slender, anterior canal; outer lip, widely expanded for-
ward, retractive above into a deep sinus lying in the sutural
fasciole.
Length, 62.0 mm.; diameter, 18.5 mm.; aperture, 34.0 mm.
This species resembles the Turris (Surcula) fusinella Dall”
which is the type of Woodring’s Fusiturricula.’* The holotype
of T. fusinella is an immature specimen having a length of only 17
mm., dredged in the Gulf of Panama at a depth of 153 fathoms.
Type.—Paleontological Research Institution, No. 4037.
Occurrence.—Charco Azul.

Genus TURRICULA Schumacher

Turricula dulcia, n. sp. Plate 7, figs. 3, 6

The shell is similar to Turriculaf#ammea Schumacher but 1s
more slender with a less strongly contracted body whorl; solid,
fusiform with a long, pointed, sharp spire having a strongly con-
tracted or concave anal fasciole, nearly 4% the spire whorl in
width, less wide in proportion on the penultimate whorl; sutures
appressed ; the surface is generally smooth, except on the whorls
of the spire which show a series of ribs on the fasciolar angle to
the number of about It on each turn but fade out so that they
are practically lacking from the last whorl; on the body whorl,
the surface is nearly smooth except for fine spiral lines which
appear on magnification, much stronger on the base of the last
whorl and on the canal; aperture narrow, elliptical produced for-
ward into a long canal, slightly bent; pillar, thick, solid and
smooth; outer lip arcuate in the lower part, with a deep, anal
sinus lying in the sutural fasciole.

18 Dall, W. H.: The Albatross Report, 1908, p. 261, pl. 14, fig. 7.

19 Woodring, W. P.: Miocene mollusks from Bowden, Jamaica, Car-
negie Inst. Washington, Pub. No, 385, 1928, p. 165.

207 BuricA PENINSULA FOoSssILs: OLSSON EY)

Length, 47 mm.; diameter, 16 mm. ; aperture, 24 mm.

This shell is quite similar to Turricula flammea Schumacher,”
the type of the genus Turricula, but is more slender with a less
strongly contracted body whorl. The Twrricula libya Dall?’
from San Lucas is a stouter and shorter shell with stronger
sculpture. Another similar species is the Surcula nelsoni Olsson**
from the Tumbez beds of northern Peru but that species is larger
and entirely lacking in ribs.

Type.—Paleontological Research Institution, No. 4038.

Occurrence.—Quebrada Penitas.

Subgenus KNEFASTIA Dall

Turricula (Knefastia) andesita, n. sp. Plate 7, fig. 8

Shell rather large, coarsely sculptured, principally with spirals,
the ribs being practically absent; nucleus unknown, about 8, post-
nuclear whorls preserved; sutures very indistinct; the whorls are
moderately convex, with the sutural fasciole hardly differenti-
ated, this part of the whorl being merely constricted and without
any marked change in sculpture; in the sculpture, the axial ribs
are practically absent but with slightly irregular undulations
marking former stages of rest; the spiral sculpture is strongly
developed and consists of spiral cords, heaviest about the periph-
ery, weaker in the zone of the sutural fasciole and separated by
wide intervals carrying finer, secondary threads; on the spire
whorls, there are about 5, principal spirals, increased to about 20
on the body whorl; the principal spirals begin at the lower margin
of the sutural fasciole and extend to the tip of the anterior canal;
spiral interspaces have generally 4, fine spiral threads; anal sinus,
deep, lying in the middle of the sutural fasciole; aperture and

canal imperfect but apparently the canal was moderately long,
Fusus-like.

20 In Grant, U. S. IV, and Gale, H. R.: Pliocene and Pleistocene
Mollusca of California, Mem. San Diego Soc. Nat. Hist., vol. 1, 1931, p.
486, pl. 25, figs. 9a, 9b.

22 Dall, W. H.: Proce. U. S. Nat. Mus., vol. 56, 1919, p.-2, pl. 2, fig. 5.

22 Olsson, A. A.: The Peruvian Miocene, Bull. Amer. Paleont., vol. 19
1932, p. 150, pl. 16, fig. 10.

56 BULLETIN 106 208

Length, 47.0 mm.; (imperfect), diameter, 19.5 mm.; aper-
ture, 16.0 mm. (imperfect).

Related to Turricula lavinia Dall?* from the West Coast of
Mexico, this species differs by its stronger sculpture and less well-
defined sutural fasciole. The sculpture of strong spiral cords, their
intervals sometimes finely etched by the lines of growth, resem-
bles that of the more finely sculptured species of Polystira but the
retral sinus is that of Turricula and lies in the middle of the
sutural fasciole. The ribs are practically absent but there is a
series of irregularly spaced undulations, the larger ones marking
stages of rest in the growth of the shell.

Type.—Paleontological Research Institution, No. 40309.

Occurrence.—Charco Azul formation, basal sands, mouth of
Quebrada Penitas.

Genus PLEUROTOMELLA Verrill
Subgenus PHYMORHYNCHUS Dall
Pleurotomella (Phymorhynchus) agina, n. sp. Plate 10, fig. 10

Shell of small or medium size, elongate-fusiform or columbel-
loid in form, smooth, polished; upper part of spire broken; su-
tures appressed, the whorl in front of it slightly constricted form-
ing a shallow sutural fasciolar band; surface appearing smooth
but on magnification showing fine, more or less, irregular spiral
lines covering the anterior canal and the face of the body whorl
except the sutural fasciole which is entirely smooth or marked
with much finer, spiral lines; aperture semielliptical, the outer
lip thin, arched forward in the middle, retractive towards the
suture to form a shallow anal sinus adjacent to the suture; canal
of moderate length, a little recurved at the tip.

Length, 27.50 mm.; diameter, 13.50 mm.; aperture, 15.00 mm.

This species is quite similar to the Pleurotoma (Surcula)
dissinulis Watson,** dredged off the southeast side of the Philip-
pines in 500 fathoms. The Philippine shell is larger (2.65 inches
or about 67.50 mm.) and the sculpture is somewhat coarser but
the shape is very similar. The Panama shell may also be com-

23 Dall, W. H.: Proc. U. S. Nat, Mus., vol. 56, 1919, p. 4, pl. 1, fig. 6.

24 Watson, R. B.: Report on the Scaphopoda and Gasteropoda, II, Re-

port on the Scientific Results of the Voyage of the H. M. 8S. Challenger,
Zo6l. vol. 15, 1885, p. 298, pl. 26, fig. 3.

209 BuricaA PENINSULA FOSSILS: OLSSON 57

pared with the Pleurotomella (Phymorhynchus) argeta Dall?

dredged in 812 fathoms of water, near the Galapagos.
Type—Paleontological Research Institution, No. 4040.
Occurrence.—Charco Azul.

Genus LEUCOSYRINX Dall
Leucosyrinx nicoya, n. sp. Plate 12, fig. 2

Shell thin, with a high, conic spire of 7 or more whorls, the
apex and nucleus eroded; sutures appressed to slightly chan-
nelled ; the whorls are strongly carinated at a point about one-third
the whorl interval above the lower suture; above the peripheral
carina, the surface is flattened, sloping, marked with fine spirals
and the deeply arcuated growth lines of the anal sinus lying in
about the middle of this area; below the peripheral angle, the
surface has coarse, spiral cords or threads, somewhat alternating
in strength; canal and lower part of the aperture not known.

Length, imperfect about 21 mm.; diameter, 17 mm.

We have fragments of 2 specimens of this species, both lack-
ing the anterior portion. L. persimilis Dall?* dredged from a
depth of 1020 fathoms in the Gulf of Panama, is more slender.

Type.—Paleontological Research Institution, No. 5013.

Occurrence.—Charco Azul.

?Leucosyrinx buricana, n. sp. Plate 12, fig. 3

Shell of medium size, thin, volutiform, the spire and canal of
about equal length; nucleus unknown, subsequent whorls 4 or
more; sutures appressed; the whorls are narrowly shouldered,
bearing a series of small, curved riblets which begin at about
the middle zone of the body whorl but do not reach the upper
sutures ; on the body whorl, the riblets number about 14; besides
the axial riblets, the sculpture on the body whorl consists of about
19, flat, spiral bands between impressed lines which begin on the
canal and continue to the shoulder or edge of the sutural fasciole
which is smooth; aperture elliptical, the outer lip thin; the anal
sinus 1s very broad and shallow; anterior canal is moderately
wide and nearly straight.
ee Dall We es) Proc) U.S. Nats Muse) voli il2" 1889) 3077. pole (oy Gaiters ye
Dall, W. H., The Albatross Report, 1908, p. 283, pl. 19, fig. 8.

> ?
26 Dall, W. H.: The Albatross Report, Bull. Mus. Comp. Zool., vol. 43,
NO mo ONS Sipe aeolian los fiom. 2

58 BULLETIN 106 210

Length, 38.00 mm. ; diameter, 20.00 mm. ; aperture, 24.50 mm.

This species is not a typical Leucosyrinx but is referred to that
genus tentatively because of its likeness to ’Leucosyrinx galapag-
ana Dall. The shell is poorly preserved and eroded but has the
appearance of a deep-water species.
?Leucosyrinx galapagana Dall®’ dredged in 634 fathoms off the
Galapagos Islands by the U. S. Bureau of Fisheries steamer Al-
batross is somewhat like our species but is smaller and more slen-
der.

Type.—Paleontological Research Institution, No. 5014.

Occurrence.—Charco Azul.

Genus BORSONIA Bellardi
Subgenus BORSONELLA Dall
Borsonia (Borsonella) adamsi, n. sp. Platem2eenceeet

Shell of medium size, biconic, the aperture and spire of about
equal length; apex eroded but with about 6 remaining whorls ;
the whorls are white or faun colored, polished but generally
somewhat corroded; sutural fasciole well marked but not deep,
forming a sloping or excavated band, a little more than half the
width of the spire whorls and ornamented with flattish, spiral
bands ; shoulder with sloping, oblique ribs which on the last whorl
number about 15: these ribs are absent from the sutural fasciole
and from the base; whole surface covered with low, smoothish,
spiral bands, the lined interspaces of which may be beaded; anal
sulcus lying at the anterior side of the fasciole is moderately deep ;
aperture wide, the pillar with a single, obscure fold, the anterior
canal slightly twisted.

Length, 27 mm.; diameter, 17 mm.; aperture, 14.5 mm.

This species is like Borsonella agassizti Dall?® dredged from a
depth of 1471 fathoms in the Gulf of Panama by the Albatross
but has a longer canal and stronger axial sculpture. Like most
of the other turrids from Charco Azul having deep-water char-
acteristics, our shells are somewhat corroded and imperfect. It
is possible that they had drifted some distance to their present

Dall W. H.: Proce. U. S. Nat. Mus., vol. 56, 1919, p. 5, pl. 3, fig. 2.

ies Dall, W. H.: The Albatross Report, Bull. Mus. Comp. Zo6l., vol. 43,
No. 6, 1908, p. 275, pl. Ly fic. 5.

Dalal BuricA PENINSULA FossiLs: OLSSON 59

station but many deep-water mollusks show naturally the effects
of water corrosion.
Named for C. B. Adams, pioneer student of Panama shells.
Type.—Paleontological Research Institution, No. 5010.
Occurrence-—Charco Azul.

Borsonia (Borsonella) harrisi, n. sp. Plattemt arate SemG sul

Shell small, biconic, the aperture and canal of about equal
length; nucleus unknown, the remaining whorls 6 or 7 in num-
ber; the sutural fasciole forms a well-marked, sloping or exca-
vated, smooth band which is about half the width of the spire
whorl; surface below the fasciole is strongly sculptured with
oblique riblets and spirals; the ribs are strongest just below the
shoulder and number about 21 on the last whorl; the spirals form
strong, flattened cords, separated above by incised lines only, and
by deeper grooves on the base and canal; anal sulcus lying in the
fasciole is quite wide; aperture wide, the pillar nearly straight,
unarmed ; anterior canal slightly twisted.

Length, 14.5 mm.; diameter, 6.8 mm.

Length, 15 mm.; diameter, 6.75 mm.

This is a smaller species than B. adamsi, the columella being un-
armed in our two specimens.

Type.—Paleontological Research Institution, No, 5011; other
specimen, No. 5012.

Occurrence.—Charco Azul.

Family CANCELLARIIDZ

Genus CANCELLARIA Lamarck

Subgenus CANCELLARIA, s. s.
Cancellaria (Cancellaria) penita, n. sp. Plate 8, figs. 4, 8
Shell of medium size, ovate to subpyriform, the body whorl
usually large, with the earlier whorls forming a smaller, conic,
pointed spire; the nucleus is small, eroded on our specimens,
followed by 6 or 7, postnuclear whorls; sutures excavated to
narrowly channelled; sculpture consists of equal, spiral cords
separated by much wider interspaces and a series of somewhat
finer, longitudinal riblets which feebly nodulate the spirals at their
intersections ; on the penultimate whorl, the principal spirals num-
ber 6 between the sutures, in addition to a smaller spiral thread

bo

60 BuLLETIN 106 Pali

about the upper suture; on the last whorl, there are about 19
principal spirals, somewhat wider spaced above, and a little
crowded on the anterior canal; umbilicus absent, the anterior
canal produced, sometimes slightly perforate with a small, ex-
ternal cordlike fold; aperture semielliptical, the outer lip not
thickened, toothed or dentated by the spiral sculpture, internally
with a series of long, slender liree which extend deeply into the
throat of the shell; inner lip with a thin wash of callus which does
not entirely conceal the sculpture, the columella straight, pro-
vided with 3 folds, the posterior one being the largest; small,
varices, scarsely distinguishable, are developed on the back of
some turns as small swellings.

Length, 27.00 mm.; diameter, 18.00 mm. ; aperture, 18.50 mm.

From Cancellaria dariena Toula, this species differs by its
larger body whorl, smaller spire so that the shape is pyriform.
Cancellaria cominella Pilsbry and Olsson which is based on a
young shell from the Pliocene of Ecuador is quite similar but
has a higher spire.

Type.—Paleontological Research Institution, No. 4041; other
specimens, No. 4042.

Occurrence.—Quebrada Penitas.

Subgenus BIVETOPSIS Jousseaume

Cancellaria (Bivetopsis) charapota, n. sp. Plate 8, fig. 3

Shell of medium size, solid, sculptured with scabrous ribs and
spirals ; aperture ovate, the outer lip somewhat thickened, appear-
ing as if widely fluted just below the middle and closely lirated
within; inner lip with a callus shelf, irregularly pustulated on the
outer portion and with strong lirze in the interior; the spire is
rather short, of about 5 whorls (apex lost) and only about half
the length of the rest of the shell; sculpture consisting of nar-
row, retractive axial ribs which are rendered scabrous by the
spirals and on the shoulder become somewhat spiniferous ; on
the last whorl, these ribs number about 10, the last one on the
outer lip becoming greatly enlarged; there are 12 spiral threads
between the shoulder angle and the fasciolar cord, and there are

3 or 4 more on the area above the shoulder; columella excavated
« c c ’

with 3 plaits, the middle one being the smallest; siphonal canal

213 BuricA PENINSULA Fosstns: OLSSON 61

short and strongly recurved, developing into a prominent cord on
the back.

Length, 22 mm.; diameter, 17 mm.

This small species is quite common in the middle Miocene
silty sandstones at Punta Charapota about midway between
Manta and Bahia on the west coast of Ecuador.

Type.—Paleontological Research Institution, No. 4043.

Subgenus CHARCOLLERIA, new subgenus

yenotype.—Cancellaria perdiciana, n. sp.

The following is a description of the subgenus Charcolleria.

The shell is fusiform having the spire and aperture of about
equal length, narrowly umbilicate, the base of the body whorl
somewhat contracted at a point opposite the upper part of the
aperture; anterior canal a little curved backwards, the siphonal
sinus giving rise to an angled ridge forming the upper side or
edge of the umbilicus; columella with 2 plaits, the upper one the
larger ; sculpture evenly reticulated ; the outer lip with a shallow,
stromboid notch.

Cancellaria (Charcolleria) perdiciana, n. sp. Plate 8, fig. 5

Shell large, fusiform, solid; spire high of about 5 or more
strongly convex whorls, the spire and aperture being of about
equal length; anterior canal with a narrow, deep umbilicus,
bounded above by a sharp keel, beginning at the upper columellar
fold; the sculpture is finely reticulate, resulting from the inter-
section of fine, spiral threads and small wrinklelike, axial riblets ;
on the spire whorls, the spirals number about 11, their interspaces
being wider; on the last whorl, there are about 22 spirals count-
ing from the umbilical angle to the upper suture; aperture semi-
elliptical, with a slightly recurved, anterior canal at its tip; pillar
straight, callused and with 2 strong plaits, the upper one being
the larger.

Length, 60.00 mm. ; diameter, 28.50 mm.; aperture, 30.00 mrh.

The present species is found in the Las Perdices shales of
northern Colombia and is described in this place for comparison
with Cancellaria terryi from Panama. The Colombian shell is
perfect and has a well-developed umbilicus and it differs mainly

62 BULLETIN 106 214

from the Panamanian species by its finer reticulate sculpture.
Type.—Paleontological Research Institution, No. 4044.
Occurrence._-Las Perdices shales, Puerto Colombia. Lower
Miocene.

Cancellaria (Charcolleria) terryi, n. sp. Plate 8, fig. 1

Shell fusiform, solid. with a high spire of about 6, strongly
convex whorls; the nucleus is missing; body whorl relatively
small, convex, extended forward into the fusiform anterior canal ;
sculpture is coarsely reticulate, formed by strong, spiral cords
between wider interspaces and a series of small, axial riblets of
the same strength as the spirals; on the spire whorls, there are
about 9 spiral cords while on the body whorl they number be-
tween 17 or 18; the shell was perhaps umbilicate or became so
at maturity, but the tip of the anterior canal is broken; aperture
semicircular, the columella straight, strong, with 2 heavy plaits,
the upper one being the larger.

Length, 41.00 mm. (imperfect) ; diameter, 23.00 mm.,, aper-
ture, 18.00 mm.

The holotype 1s imperfect, having lost the tip of the anterior
canal so that the above measurements should be increased by 5
or 6 millimeters. The shell appears to have had a small, narrow
umbilicus.

Type.—Paleontological Research Institution, No. 4045.

Occurrence.—Charco Azul formation, Quebrada _ Penitas.
North fork of Rio Guanabanon.

Subgenus CALCARATA Jousseaume

Cancellaria (Calcarata) peninsularis, n. sp. Plate 10) fiewnd

Shell muriciform, solid with 5 whorls preserved, nucleus lost;
spire subtabulated, pointed, the whorls shouldered and _ strongly
sculptured ; the sculpture of the spire whorls consists of 4, spiral
cords, the 2 lower being strongest, leaving the band next to the
shoulder angle smooth, and a series of strong, varixlike ribs,
sometimes becoming spiniferous on the shoulder; on the body
whorl, there are 13 or 14 spirals, somewhat alternating in
strength and about 8 ribs; on the space above the shoulder, the
surface is smooth but with the ribs continuing across to the su-

Ale Burica PENINSULA Fosstus: OuSSON 65

ture generally in a sinuous course; aperture wide, subtriangular,
the outer lip apparently smooth within, the columella bearing 3,
strong plaits and small irregular pustules.

Length, 31 mm.; diameter, 19 mm.; aperture, 17 mm.

Our shell is imperfect, somewhat weathered and is not fully
mature. It is apparently related to Cancellaria centrota Dall**
described from near Cocos Island, Bay of Panama. It differs
from Dall’s figure and description of C. centrota in being imperfor-
ate, has a higher spire, less spiniferous shoulder varices and in
having a greater number of spiral cords on the body whorl.

T ype—Paleontological Research Institution, No, 4046.

Occurrence.—Quebrada_ Penitas.

Cancellaria colombiana, n. sp. Plate 9, fig. 4

Shell of medium size, stout; nucleus not preserved, succeed-
ing whorls number 5 or more; the spire is elevated, scalar, with
a deeply excavated sutural zone; the sculpture is sharply or
nodosely reticulated and is formed by the intersection of strong,
narrow, oblique riblets and coarse spirals; on the last whorl, the
ribs number about 12, these are fairly uniformly developed over
the greater part of the shell but tend to become enlarged and
irregular on the back of the last whorl; spiral sculpture is formed
by relatively few, strong cords; on the spire whorls, one of these
cords forms the sharp angle of the shoulder, with 2 spirals below
it and 2 smaller ones along the edge of the deeply excavated, su-
tural zone; on the last whorl, there are about 12 spirals below
the shoulder; a narrow umbilicus is developed but it is not bor-
dered by any noticeable keel or cord; aperture semilunate; the
outer lip not strengthened in type (shell may not be quite ma-
ture) and with about 14, long, deeply entering lire; columella
straight with 3 folds of which the posterior one is the strongest ;
anterior canal short, ending in a straight, siphonal canal.

Length, 33.5 mm.; diameter, 23 mm.

The subgeneric relations of this interesting species is not
known. It is characterized by its straight and not recurved
siphonal canal deeply excavated sutural zone and a reticulated

29 Dall, W. H.: The Albatross Report, Bull. Mus. Comp. Zo6l., vol. 43
No. 6, 1908, p. 295, pl. 1, fig. 8.

64 BULLETIN 106 216

sculpture rendered sharply nodose by the intersection of the
narrow, strongly oblique ribs and coarse spirals. Only the type
specimen is known which comes from the Upper Las Perdices
shales at Puerto Colombia Its age is probably lower Miocene.
Type.—Paleontological Research Institution, No. 4047.

Family MITRIDZ
Genus MITRA Martyn
Mitra cyclica, n. sp. Plate 7, fig. 1

Shell of medium size, rather solid and strongly sculptured:
the spire, with 7 whorls (apex lost) preserved on our specimen,
is pointed and about the same length as the aperture and an-
terior canal; sutures are well marked and deeply grooved with
the surface of the whorl between flattened to slightly convex;
the sculpture is formed by strong, spiral cords between deep,
encircling grooves; on the holotype, these grooves are mainly
smooth except on the spire whorls where they are etched by deep,
longitudinal lines; on the penultimate whorl there are 4 spiral
cords; on the last whorl, there are 12 spiral cords and about 4
more on the canal; aperture narrow, the outer lip solid but not
thickened, frilled by the ends of the spiral cords; columella with
4 plaits, the anterior one being quite small.

Length, 50 mm.; diameter, 16 mm.

Only the type specimen is known. The shell is solid and
strongly sculptured with large, prominent spiral cords separated
by deep spiral grooves. The fossil appears to be closely related
to the rare Mitra belcheri Hinds from the Gulfs of Nicoya and
Papagayo. Judging by Reeve’s figure, Mitra belcheri is a more
slender species with a longer spire and shorter, stouter body
whorl. In Mitra belcheri, 5 cords are fully visible on the pen-
ultimate whorl while in the fossil there are but 4.

Type.—Paleontological Research Institution, No. 4048.

Occurrence.—Quebrada Penitas.

Family FASCIOLARIIDZE
Genus LATIRUS Montfort
Latirus penitus, n. sp. Plate 8, fig. 10

Shell of medium size, fusoid, the spire and aperture of equal
length; nucleus unknown, the succeeding whorls of the spire
numbering about 7, are convex and provided with knobbed ribs,

217 Burica PENINSULA FOSSILS: OLSSON 65

strongest in the middle; the ribs number about 8 on the last turn,
progressively less on the earlier ones, these ribs are strongly
developed in the middle but are absent from the base and from
the zone bordering the suture; on the whorls of the spire, the
ribs are crossed by 3 prominent spirals, separated by very wide
interspaces which generally carry a single, secondary thread
and occasionally smaller tertiary ones, especially in sutural inter-
space; in addition, the whole surface of the shell is sculptured
with fine, longitudinal threads; on the base of the last whorl, the
spirals are more irregular and cannot be classified easily into
primaries and secondaries; aperture semilunate above, drawn-
out and narrowed below; outer lip with 7 long, entering lire;
columella with 3, small plaits; anterior canal, long, slightly twist-
eae

Length, 53 mm.; diameter, 21 mm.; aperture, 28 mm.

This species resembles Latirus varicosus Reeve but is distin-
guished by its slender form and in having the spire and anterior
canal of nearly equal length.

Type.—Paleontological Research Institution, No. 4040.

Occurrence.—Quebrada Penitas.

Genus FUSINUS Rafinesque

Fusinus mellisus, n. sp. Plate 9, fig. 7

Shell rather large, solid; the specimen is broken but originally
the spire and aperture (including the anterior canal) was prob-
ably of equal length; 6 whorls are preserved but the nucleus and
earliest spire whorls are lost; axial sculpture of the whorls of
the spire is formed by 6, prominent rounded ribs with about
equal interspaces; on the last whorl, the ribs have increased to
10; on the spire whorls, the ribs cross from suture to suture but
later become more confined to the periphery and on the last
whorl are obsolete in the sutural zone and from the base; suture
is somewhat appressed; spirals cover the entire surface and con-
sist of the usual threads of slightly different strength, a
set of primaries, widely spaced with a central secondary which
is bordered on each side by still smaller tertiary threads; on a
whole, the spirals are quite uniform over the entire surface and
the peripheral one does not become noticeably stronger than the

66 BULLETIN 106 218

others; outer lip simple, broken in our specimen; inner lip with
a thin spread of callus; anterior canal long, broken in specimen.

Partial measurements are as follows:

Length, 82 mm.; diameter, 35.5 mm.

Dall?’ has described Fusinus panamensis from the Gulf of
Panama, depth 153 fathoms, but the species has remained unfig-
ured and we have had no opportunity of examining the type.
The descriptions and measurements of /*. panamensis indicate
a shell of quite different characters.

Type.—Paleontological Research Institution, No. 4050.

Occurrence.—Quebrada Mellisa.

Fusinus, sp.

This record is based on a single fragment of about 3 whorls.
Each turn has 8 ribs further marked with 8 primary spirals and
smaller secondaries.

Occurrence.—Burica Point.

Family BUCCINIDA
Genus HANETIA Jousseaume
Hanetia pelicana, n. sp. Plate 3, fig. 3

Shell solid, muricid, with a sculpture of thick ribs and coarse
spirals ; spire high, conic, about one-half the total length; whorls
about 5% (tip missing) ; axial sculpture is formed by 5, strong,
thick ribs between wider interspaces; on the spire whorls, the
ribs extend from suture to suture but on the last turn do not pass
much below the upper quarter of the aperture, except the last rib
which forms the back of the outer lip; spirals consist of coarse,
alternating threads, there being about 9 primary threads on the
penultimate whorl in the space between the sutures ; aperture oval,
outer lip bowed with about 18 lire within, inner lip smooth; canal
short, wide, recurved at the end.

Length, 38 mm.; diameter, 21 mm.; aperture, 21 mm.

This species is nearest to H. elegans Dall*’ but has a higher
spire and fewer ribs. Known only from the holotype which is
imperfect.

Type.—Paleontological Research Institution, No. 4051.

Occurrence.—Burica sandstones, Burica Point.

30 Dall, W. H.: Bull. Mus. Comp. Zodl., vol. 43, No. 6, 1908, p. 301.
%1 Dall, W. H.: The Albatross Report, 1908, Bull. Mus. Comp., Zo6l. vol.
43, No. 6, 1908, pp. 300, 301.

219 Burica PENINSULA FOossILsS: OLSSON 67

Hanetia anomala burica, n. subsp. Plate 11, fig, 2

Shell of medium size, solid, subfusiform with a conic spire
equal to the aperture in length; whorls 54 (tip missing), the
last whorl strongly angled or shouldered in the middle; sculp-
ture is formed by thick, foldlike ribs, strongest on the middle or
shoulder, and numbering about 7 on the last whorl, crossed by
strong, spiral cords (which are generally formed by 3, finer,
spiral threads) separated by deeply concave interspaces; these
cords number 6 on the penultimate whorl; on the last whorl, there
are 4 of these spirals on the area between the suture and the
shoulder, 10 or 11 on the area between the shoulder and the um-
bilical keel; a strong keel rising in the notch of the anterior sinus
surrounds the umbilical area which is sculptured principally by
irregular growth lines; aperture subelliptical, the outer lip den-
ticulated by the ends of the spiral cords and lirated within.

Length, 49 mm.; diameter, 36 mm.; aperture, 31 mm.

From the Recent species, this form differs by its fewer ribs
and more strongly ribbed shoulder.

Type.—Paleontolozical Research Institution, No. 4052.

Occurrence.— Quebrada Mellisa.

Subgenus FUSINOSTEIRA Olsson
Hanetia (Fusinosteira) alternata Nelson Plate 10, fig. 1

Cuma alternata Nelson, 1870, Trans. Conn. Aead. Sei., vol. 2, p: 1985 pl:
fangs. 3, 4.

Solenosteira alternata Spieker, 1922, Johns Hopkins Uniy. Studies Geol.,
No. 3, p. 45, pl. 1, figs. 10, 11.

Solenosteira (Fusinosteira) alternata Olsson, 1932, Bull. Amer. Paleont.,
vol. 19, p. 181.

This large and perhaps the finest of the described species of
Hanetia was previously known only from the type specimens
collected in the Tumbez beds of northern Peru, Nelson’s types
in the Peabody Museum, Yale University, were loaned to me for
study through the kindness of Dr. Dunbar. The Peruvian spec-
imens differ in no way from the Panamanian except that the
latter are more perfectly preserved. The shell is large, fusiform,
shouldered and strongly sculptured with ribs and spirals. On
the last whorl, the ribs number about 8. They are strongest on
the angle of the shoulder, fade out above and extend below only

68 BULLETIN 106 220

as greatly reduced, wavelike folds to about the middle of the base
or about halfway from the shoulder angle to the ridge bordering
the umbilicus. Spirals are more or less alternating in character.
They usually consist of a primary set between which there are
3 smaller ones so that the spiral sculpture as a whole appears
banded. The umbilicus is deep and narrow, bounded above b,
a sharp, keel-like fold. Aperture subovate, produced anteriorly
into a strongly recurved canal. The outer lip is thin, smooth
or lirated feebly within, slightly sinuous in profile.

Length, 74 mm.; diameter, 47 mm.; aperture, 46 mm.

This species is common at Charco Azul where several beau-
tiful specimens were obtained. It is rare in Quebrada Penitas
associated with Acila isthmica burica and Strombina fusiformis
penta.

Figured specimen.—Paleontological Research Institution, No.
4053.

Occurrence.—Charco Azul; Quebrada Penitas.

Hanetia elegans Dall

Solenosteira elegans Dall, 1908, Albatross Report, p. 300, pl. 5, fig. 6.

Our shell is not quite mature, the outer lip being scarsely
thickened and only weakly lirated within. Dall’s type was
dredged in Panama from a depth of 153 fathoms off mud bottom.

Our fossil was collected from the zone of unconformity im-
mediately beneath the basal Armuelles conglomerate at Punta de
‘Piedra. The underlying Charco Azul shales are deeply brecci-
ated and their fissures filled with fossiliferous sand. which was
introduced during the initial advance of the Pleistocene sea.

Occurrence.—Punta de Piedra.

Genus CANTHARUS (Bolten) Reading
Cantharus amycus, n. sp. Plate Wee

Shell of medium size, solid with strongly shouldered whorls ;
apex of the shell is lost but with 344 whorls remaining; the
sharply angled shoulder is ornamented by small but strong ribs
numbering about 14 on the last whorl; these ribs are practically
confined to the shoulder or only feebly developed in the sutural
area above; strong spirals cover most of the surface of the shell ;
there are about 19, primary spirals between the shoulder angle
and the weak fasciolar fold at the tip of the anterior canal; be-

22 Burica PENINSULA Fosstts: OLSSON 69

tween the primaries, there are finer secondary and ‘tertiary
threads; the interior of the shell is filled with a pebbly matrix
so that the columella cannot be seen; anterior canal of medium
length, slightly recurved at the end and with a weak fasciolar
cord.

Length, 44 mm.; diameter, 29 mm.

The question as to the true generic position of this species
will remain unsolved until specimens showing the interior are
known.

T ype.—Paleontological Research Institution, No. 4073.

Occurrence.—Burica sandstones, Burica Point.

Genus METULA H. and A. Adams
Metula pilsbryi, n. sp. Plate 9, fig. 8

Shell relatively large, stout, with the aperture more than half
its length and with a coarse but regular cancellated sculpture ;
the spire whorls number about 6 (tip missing), slightly convex
in profile; the last whorl is produced forward to form the mod-
erately long, stout anterior canal; sculpture coarsely and regu-
larly cancellated by nearly even ribs and spirals, their intersec-
tions being slightly nodose; the spiral cord adjacent to the up-
per suture is somewhat larger than the others; on the penulti-
mate whorl, the spiral number about 12; lip thickened on the
outside, slightly sinuous and feebly denticulated within; a thin
wash of callus is spread over the columellar wall; anterior canal
wide at its end.

Length, 45 mm.; diameter, 18 mm.; aperture, 20 mm.

This is a large, coarsely cancellated species. From the Recent
species, /. amosi Vanatta, also found in the Pleistocene of Pan-
ama, this species differs by its wider shell and in having the aper-
ture more than half the length of the entire shell. Our specimen
shows faint traces of the original color, in the form of broad
white and brown bands.

Type.—Paleontological Research Institution, No. 4062.

Occurrence.—Rio LaVaca and Rio Guanabanon.
Metula amosi Vanatta Plate 9, fig. 9

Metula amosi Vanatta, 1913, Proe. Acad. Nat. Sci. Phila., vol. 65, p. 22,
text figs, jl, 2:

bo

70 BULLETIN 106 22

This Recent Panamic species is quite common in the Pleisto-
cene dredgings from the Panama Canal at Thatcher’s Ferry from
which a specimen is here figured for comparison with M. pils-
bryi. On the Burica Peninsula it occurs as a Pleistocene fossil
at Rabo de Puerco and at the mouth of the Rio Guanabanon. The
figured specimen measures, length, 44 mm.; diameter, 14 mm. ;
length of aperture, 23 mm. ‘The largest specimen from Thatcher
Ferry has a length of 46 mm. and is proportionately a little nar-
rower than the one figured.

Figured specimen.—Paleontological Research Institution, No.
40632.

Family NASSIDA®
Genus NASSA Lamarck
Subgenus UZITA H. and A. Adams
Nassa (Uzita) terryi, n. sp. Plater 8) fitsse2aieno

Shell of medium size, generally white or glassy in color;
nucleus (eroded on the type), is followed by 5 whorls which are
strongly sculptured with cordlike spirals, coarsely beaded by
longitudinal riblets; on the whorls of the spire, the spiral sculp-
ture is formed by 32 strong, equal cords separated by deep, wide
intervals, sometimes with a 4th spiral showing in the lower su-
ture and a small secondary thread borders the upper one; on the
body whorl, there are 7 spiral cords between the fasciole and
the upper suture; axial sculpture consists of about 21 riblets
which extend from the fasciolar sulcus to the upper suture and
strongly nodulate the spiral cords at their points of intersection ;
aperture broadly subelliptical, the outer lip thickened by the last
rib, strongly crenulated within by about 10 teeth or slender lire
which extend deeply into the throat of the shell; inner lip with
a platform of callus, smooth or with a few, small, scattered pus-
tules; beak rather long, encircled by a shallow sulcus; anterior
canal is moderately long, wide, slightly recurved, its edge bound-
ed by a strong keel-like plait.

Length, 22.5 mm. ; diameter, 13.5 mm. ; aperture, 10.5 mm.

Some of the shorter specimens resemble the Nassa miser Dall
(Albatross Report, p. 307, pl. 4, fig. 1) from the Gulf of Panama
but the fossils are generally longer, the anterior beak is less
stubby and is encircled by a shallower, fasciolar sulcus, They

223 BuricA PENINSULA Fossius: OLSSON (fl

also differ notably in sculpture. This species is the commonest
fossil at Charco Azul.

Type—Paleontological Research Institution, No. 4054; other
specimens, No. 4055.

Occurrence.—Charco Azul.

Nassa (Uzita) armulla, n. sp. Pita 8, fig. 6

Shell of medium size with about 9, reticulately sculptured
whorls; nucleus small, pointed, its surface being eroded on the
type specimen; the postnuclear whorls, a little convex in form,
except the last which is strongly convex; sutures well marked ;
the sculpture consists of strong, cordlike spirals numbering about
6 on the spire whorls, the lowest one being almost concealed in
the suture; on the body whorl, the spirals number about 13 from
the anterior fasciole to the suture; in addition to the spirals,
there is a series of narrow riblets which are strongly developed
over the whole shell; these riblets number about 21 on the body
whorl in addition to a stronger rib which thickens the outer lip;
beak small, encircled by a deep, sulcuslike fasciole; aperture
broadly elliptical, with a well-marked posterior sinus and a deep,
recurved anterior canal; outer lip thickened by an external rib,
lirated within by fine, alternating threads, the primary ones, 13
in number; inner lip with a cover of callus bearing a set of
small plaits or lire on the parietal wall; a strong keel is placed
at the edge of the anterior canal.

Length, 21.5 mm.; diameter, 10 mm.; aperture, ITI mm.

This is a strongly sculptured species. The spire is about half
the length of the shell which has a pointed, conical spire and a
moderately large, convex body whorl.

Type.—Paleontological Research Institution, No. 4056.

Occurrence.—Charco Azul. r

Genus CYMATOPHOS Pilsbry and Olsson
Cymatophos panamensis, n. sp. Plate 9, fig. 1

Shell rather large, fusoid with a spire somewhat longer than
the aperture ; nucleus small, pointed of 3, smooth whorls; change
from the smooth, nuclear stage to the adult sculpture is gradual
by the introduction of small, threadlike lines which later develop
into the ribs; these early ribs are crossed by 2, spiral threads;

72 BULLETIN 106 224

whorls of the spire shouldered; the sculpture consists of straight
ribs which commence on the base and extend upward to the su-
ture, crossed by spiral threads, alternate in strength; the ribs
are heaviest on the whorls of the spire, extend from suture to
suture and average about 10 to each turn; spirals consist of
strong threads of primary strength, widely spaced, the inter-
spaces usually with a smaller or secondary thread; on the spire
whorls, the primaries number about 6, increase to about 12 on
the last whorl above the fasciolar keel; spiral interspaces finely
etched with longitudinal growth threads; aperture suboval, the
outer lip internally lirated; inner lip smooth, bordered by an
oblique, spiral cord; siphonal fasciole bordered by a keel-like
spiral and a moderately deep furrow.

Length, 44 mm.; diameter, 19 mm.; aperture, 21 mm.

From Cymatophos galerus Pilsbry and Olsson, this species
differs by its smaller size and coarser spirals. A single worn
specimen from the coast of Ecuador shows that the species is
living in the Recent fauna.

Type.—Paleontological Research Institution, No. 4057.

Occurrence.—Rio La Vaca.

Genus PHOS Montfort
Subgenus ANTILLOPHOS Woodring
Phos (Antillophos) gatunensis Toula

Phos gatunensis Toula, 1909, Jahrb. der K-K. Geol. Reichsantalt, Wien,
vol. 38, p. 701, pl. 28, fig. 6; pl. 25, fig. 11.

Phos gatunensis Brown and Pilsbry, 1911, Proce. Acad. Nat. Sci. Phila.,
vol. 63, p. 349, pl. 25, figs. 1, 2.

Phos gatunensis Olsson, 1922, Bull. Amer. Paleont., vol. 9, p. 289, pl.
9, figs. 4, 5.

Tritiaria (Antillophos) gatunensis Woodring, 1928, Carn. Inst. Wash-
ington, Pub. No. 385, pp. 260, 261.

One imperfect specimen of this species was collected associ-
ated with Solemya near Burica Point. A comparison with typi-
cal P. gatunensis shows only minor differences which may not
be constant in a larger series. The Burica shell is stouter and
there are some slight differences in the character of the second-
ary sculpturing.

Occurrence.— Burica formation, Burica Point.

225 BurIcA PENINSULA FossiLs: OLSSON 73

Phos (Antillophos) rutschi, n. sp. Plate 9, fig. 5
Shell of medium size, rather stout, the spire and aperture of
about equal length and a coarse, even, reticulated sculpture;
nucleus unknown; postnuclear whorls about 6; on thes ‘Spire
whorls, there are 5, spiral cords, slightly coarser below, and fine-
ly noded by the crossing of the longitudinal riblets which are
of about the same strength as the spirals themselves ; in the spiral
intervals, there is one or two, fine threads; on the last whorl, the
spiral cords number 13 or 14 between the upper suture and the
fasciolar sulcus; on the penultimate whorl, the longitudinal rib-
lets number about 27, they are more numerous on the body whorl
where they are occasionally rather closely crowded; aperture
narrow, elliptical, the outer lip somewhat thickened, bearing a
series of about 10, long lire; columella with 3 small folds or
plaits, the lower one a little stronger than the others; a small
tooth or ridge sits on the parietal wall near its posterior edge.

Length, 30 mm.; diameter, 15 mm.; aperture 1 6 mm.

Differs from P. gatunensis Toula and P. mexicanus Bose by
its stouter shell and more regular sculpture, the riblets being a
little stronger than the spirals. A somewhat similar but larger,
undescribed species is found in the La Perdices shales at Puerto
Colombia, Colombia.

T'ype.—Paleontological Research Institution, No. 4058.

Occurrence.—Quebrada Penitas, Costa Rica.

Genus MITRELLA Risso
Subgenus LONGITRELLA, new subgenus

Genotype.—Mitrella (Longitrella) vespertina, n. sp.

The following is a description of the subgenus Longitrella.

Shell of medium size to small, slender, nearly smooth except
for basal spirals; spire high; anterior canal of medium length,
quite wide and slightly recurved at end; outer lip moderately
thickened and with a series of small, irregular denticles within.

Remarks.—Differs from Mitrella in possessing a true anterior
canal and from Cosmioconcha by its more slender form, longer
canal and in sculpture.

Mitrella (Longitrella) vespertina, n. sp. Plate 10, fig. 9

Shell of medium size, with a slender spire about twice the

74 BuLLETIN 106 226

length of the aperture; nucleus unknown, subsequent whorls 8
or more; the general surface is smooth except on the base of
the last whorl and on the anterior canal which has strong spirals ;
the earliest spire whorls have also a strong, central impressed
line; aperture broadly elliptical merging forward into a rather
wide, anterior canal which is slightly recurved at the end; outer
lip moderately thickened and with a series of irregular denticles
within; inner lip and pillar smooth.
Type.—Paleontological Research Institution, No. 5014.

Charco Azul.

Genus STROMBINA Morch

Occurrence.

Strombina fusiformis penita, n. subsp. Plate 10, figs. 8, 6, 8
Shell slender, fusiform, with a long, slender, attenuated spire
of 10 or more whorls; the first 7 whorls of the spire are finely,
longitudinally ribbed, the following become shouldered, smooth
or have a series of fine spiral lines encircling the whorl around
the shoulder angle; last whorl subtriangular in transverse sec-
tion, with a strong node on the left side and a dorsal hump near
the suture or on the almost vanished shoulder; surface of body
whorl smooth except for a series of spirals on the back of the
anterior canal; aperture narrow, with a large, thickened outer
lip carrying a deep notch near the posterior end, crenulated be-
low; anterior canal produced, somewhat recurved at its end.

Length, 34 mm.; diameter, 13.0 mm.; aperture, 9.75 mm.

Length, 34 mm. ; diameter, 13.5 mm.; aperture, 9.5 mm.

This species belongs with the group of S. prisma Pilsbry and
Johnson and S. cyphonotus Pilsbry and Johnson of the Santo
Domingan Miocene and S. lessepsiana Brown and Pilsbry of
Gatun but is nearest related to S. fusiformis Hinds*? described
from an unknown locality in the Mollusca of the Voyage of the
Sulphur. The figures of Hinds and Reeve show a shell more
slender than ours, the diameter being about one-third of its
length. In the three Miocene species, enumerated above, the

dorsal hump is smaller and is bordered by small, longitudinal
folds, absent in ours.

32 Hinds, R. B.: Zoology, Voyage of the Sulphur, Mollusca, 1844, p-
38, pl. 10, figs. 17, 18; Reeve, L., Ieon., Columbella, sp. 17,

227 BuricA PENINSULA FossILs: OLSSON 75

T ype.—Paleontological Research Institution, No. 4060; other
specimens, No. 4061.
Occurrence.—Shales of Quebrada Penitas, Costa Rica.

Subgenus COTONOPSIS, new subgenus

Genotype-—Strombina (Cotonopsis) panacostaricensis, n. sp.

The following is a description of the subgenus Cotonopsis,

Shell of medium size, solid; sculpture is smooth except for
the longitudinal ribbing of the spire whorls (later becoming sub-
obsolete) and fine, irregular spiral threads; anterior canal rather
long, strongly recurved at the tip; outer lip moderately thick-
ened and feebly lirated within; pillar straight, smooth with a
single, strong or weak inner fold about midway; posterior sinus
directed upwards, bordered by a small tooth on the parietal wall;
nucleus small of 2 to 3 smooth, convex whorls.

Remarks.—This subgenus is represented by 2 species in the
Tertiary beds of the Burica Peninsula, only one being described
in this paper. From typical Strombina (genotype, S. lanceolata
Sowerby), the group differs by the circular section of the body
whorl, less thickened lip (which is not strongly denticulated
within) and in the more strongly recurved anterior canal. In
the undescribed species, the columella fold is very strong but in
the genotype it is rather small. A strong tooth borders the parie-
tal side of the posterior sinus.

Strombina (Cotonopsis) panacostaricensis, n. sp. Plate 10, fig. 5

Shell relatively large, with a high, sharply pointed spire about
equal to the aperture in length, polished, solid; nucleus small, of
about 214% smooth whorls; postnuclear whorls about 8, the first
being sculptured with longitudinal folds or ribs which gradually
become obsolete on the later turns; sutures distinct, linear; the
sculpture as noted, is formed at first by a series of straight, regu-
lar, foldlike ribs but these become subobsolete on the later turns
leaving the surface nearly smooth, except for spirals extending
from the middle of the body whorl to the tip of the anterior canal ;
on magnification, a series of faint, irregular lines can be seen
covering the entire surface; aperture narrowly lanceolate, pro-
duced forward into the anterior canal which is recurved back-

76 BULLETIN 106 . 228

ward at its tip; outer lip somewhat thickened, feebly crenate
within, with a posteriorly directed anal sinus at its junction with
the body whorl; inner lip with a spread of callus bearing a tooth
adjoining the posterior sinus.
Length, 32 mm.; diameter, 13 mm.; aperture, 16 mm.
Type.—Paleontological Research Institution, No. 4059.
Occurrence.—Tuffaceous shale, west side of the Burica Penin-
sula, about 5 niles north of Punte Burica.

Femily MURICIDAE
Genus TYPHIS Montfort

Subgenus TALITYPHIS Jousseaume
Typhis (Talityphis) costaricensis, n. sp. Plate 12, figs. 5, 8

Shell of medium size; solid; each whorl has 4 main varices
which are extended upward on the shoulder into short, stout
and somewhat appressed spines and between them also placed
on the shoulder but closer to the preceding varix, are tubes di-
rected upwards; the varix on the outer lip, strongest, expanded,
forming a wide wing which extends from the upper suture and
forward along the anterior canal which it encloses; the surface
is smooth or shows only faint, spiral wrinkles; aperture circu-
lar, continuous, its edge raised above the adjacent surface.

Length, 22 mm.; diameter, 13 mm.

This species resembles the 7. martyria Dall** from the Gulf of
California, but it is more slender and the final varix is less ex-
panded.

Type.—Paleontological Research Institution, No, 4064.

Occurrence.—Mouth of Quebrada Penitas.

Family EPITONITID
Genus EPITONIUM (Bolten) Roeding

Subgenus FERMINOSCALA Dall
Epitonium (Ferminoscala) ferminianum Dall Plate 9, fig. 6

Epitonium (Ferminoseala) ferminianum Dall, 1908, Bull. Mus. Comp.
Zool., vol. 43. No. 6, p. 316, pl. 8, fig. 8.

The fossil shell from Charco Azul seems identical with Dall’s
figure and description of this’ species. Our shell is slightly

Dall. W. H.: Lhe Albatross Report. Bull. Mus. Comp. Zo6l.. vol. 43,
Nom6, L908 spy sls pile wo. tosis

~]
~l

229 BuricA PENINSULA FOSSILS: OLSSON

larger, measuring about 41 millimeters in length (Dall’s speci-
men, length, 38 millimeter). The sculpture is evenly reticu-
lated by sharp spirals and axial lamelle, while the spiral inter-
vals and the basal disk is covered with close-set, very fine, spiral
threads,

Figured specimens.—Paleontological Research Institution, No.
4005.

Occurrence.—Charco Azul; Quebrada Pejnitas.

Family CASSIDIDZE
Genus DALIUM Dall
Dalium ecuadoriana, n. sp. Plate 9, figs. 2, 3

Shell broadly bucciniform with a blunt spire and whorls sculp-
tured with strong, circular or spiral ridges; whorls 7 or more;
nucleus unknown; sculpture consists of strong, spiral ridges be-
tween channeled interspaces; a wide, concave band encircles the
posterior side of each whorl, but it is spaced from the suture by
a band ornamented with 3 spiral cords; on the body whorl, there
are 21 spiral ridges between the beak and the edge of the fascio-
lar band and 3 above; on the penultimate whorl, there are 4
ridges below the fasciole and 3 above; the top of the circular
ridges are smooth or lined with faint spiral threads; the surface
of the whorls is polished and colored either white or brown; aper-
ture subelliptical, attenuated forward, ending in a short, slightly
twisted canal; outer lip generally thin, smooth within; inner lip
with a rather thick callus spread over the parietal wall; the sur-
face of the fasciole and the spiral interspaces have very fine stria-
tions paralleling the growth lines.

Length, 43 mm.; diameter, 20 mm.; aperture, 27 mm.

Length, 39 mm. (imperfect) ; diameter, 23.5 mm.; aperture,
23 mm.

Length, 36 mm.; diameter, 21 mm.; aperture, 23 mm.

The genus Daliwm was proposed by Dall®* for D. solidum Dall
dredged by the Blake off Granada Station in the West Indies in
576 fathoms. The Ecuadorian species resembles the figure of
D. solidum very closely and there is no doubt that they belong
to the same genus. Our shells are relatively thin and easily

84 Dall, W. H.: Report on the Mollusca, Pt. 2. Gastropoda and Scapho-

poda (The Blake Report), Bull. Mus. Comp. Zoél. vol. 18, 1889, p. 230. pl.
19, fig. 10d. '

78 BULLETIN 106 230

broken while D. solidum as its name implies is solid. None of our
specimens are perfect or have the nucleus preserved. The sur-
face of the whorls are chalky and deeply corroded on some speci-
mens.

Dalium ecuadoriana occurs with Dentalium esmeraldum and
various turrids in the Esmeraldas shales of upper Oligocene age
at Punta Gorda, a few miles west of the mouth of the Rio Esmer-
aldas in northern Ecuador where it is fairly common.

Type.—Paleontological Research Institution, No. 4066.

Occurrence.—Esmeraldas tuffaceous shales. Punta Gorda

a few miles west of the mouth of Rio Esmeraldas, Province
of Esmeraldas, northern Ecuador. Age: upper Oligocene.

Family RISSOIDA®
Genus ALVANIA Risso
Alvania bartschi, n. sp. Plate 11, fig. 10

Shell minute, broadly ovate with convex, cancellated whorls;
nucleus of about 114 well-rounded, smooth whorls; postnuclear
whorls number about 24%, these are convex and sculptured with
strong, slender ribs and spiral cords enclosing squarish pits; the
last whorl has about 14 ribs (not counting the thickened lip)
which extend from the region near the columella to the upper
suture; these ribs are crossed and rendered nodose by 6 strong,
spiral cords on the last whorl and 3 on the whorls of the spire;
suture bordered by a sloping zone wider than the interspirai
spaces; base well rounded, nonumbilicate; aperture subcircular,
outer lip strongly thickened by a narrow varix; inner lip stout,
peritreme complete.

Length, 1.25 mm.; diameter, .8 mm.

This small species resembles 4. oldroyd@ Bartsch*®® in form
but 1s nonumbilicate and differs importantly in sculpture, having
fewer ribs and spirals. It is named for Dr. Paul Bartsch, Cura-
tor of Mollusks in the United States National Museum, who has
done so much work on the smaller species of West Coast mollusks,

Type.—Paleontological Research Institution, No. 4067.

Occurrence.—Zone of unconformity at the base of the Pleisto-
cene at Punta Piedra.

35 Bartsch, P.: Proce. U. S. Nat. Mus., vol. 41, 1911. p: 360, pl. 32

ey,
7
fig. oO.

231 BuricA PENINSULA FossILs: OLSSON 79
Family NATICIDA
Genus NATICA Scopoli
Natica scethra burica, n. subsp. Plate 105 figs. 2, 7

Shell of medium size, with a moderately elevated spire and
evenly convex body whorl; whorls about 4, exclusive of the
smooth, polished nucleus of 214 turns; sutures distinct; color
white, hyaline to yellowish with no indication of color bands ;
surface nearly smooth, except around the anterior side of the
suture where there is a zone of strong, tangential, very obliquely
retractive, incised lines or wrinkles which on the type number
about 33 on the last turn; in addition there are very faint growth
lines and faint revolving lines, irregularly disposed; aperture
ovate to semicircular with a spread of callus on the parietal side;
umbilicus narrow, with an obscure rib of callus within and some-
times a second rib borders the external edge; outer lip thin,
somewhat oblique; operculum calcareous with a strong, narrow,
marginal rib bordered on both sidés by a deep groove and on
the inner side by a second, wider rib.

Length, 27.5 mm.; diameter, 27 mm.; aperture, 21 mm.

From Natica scethra Dall*® (dredged in the Gulf of Panama
from a depth of 153 fathoms), the fossil differs by its larger size,
somewhat higher spire and in the sculpture of the operculum.
Dall’s figure of the operculum shows two marginal ribs of nearly
equal size while in our shell, the outer lip is smaller.

T-ype.—Paleontological Research Institution, No. 4068.

Occurrence.—Charco Azul.

Order OPISTOBRANCHIATA
Family RINGICULID2
Genus RINGICULA Deshayes
Subgenus RINGICULELLA Sacco

Ringicula (Ringiculella) costaricensis, n. sp. Plate 6, figs. 7, 8
Shell small, solid, globose, white, composed of 4, convex whorls
forming a medium-height spire with obtuse apex; sutures dis-
tinct; surface is completely smooth, generally polished or show-
ing only faint, longitudinal, narrow lines or markings in some
specimens ; last whorl large, terminating in a very thick, wide,

86 Dall, W. H.: The Mollusca and the Brachiopoda (Albatross Rept.),
Bull. Mus. Comp. Zo6l., vol. 43, No. 6, 1908, p. 333, pl. 11, fig. 5.

10) BULLETIN 106 232

lip varix; outer lip is thickest in the middle which gives rise to
a prominent, elevated bulge; aperture ovate, widest forward;
columella with 2 strong plaits; parietal callus thick, resembling
a fold and often carrying a small tooth at its anterior end.

Length, 2.5 mm.; diameter, 2.2 mm.

This species is easily recognized by its relatively large size and
smooth, solid shell.

Type.—Paleontological Research Institution, No. 4025.

Occurrence.—Quebrada Penitas.

Class SCAPHOPODA
Genus DENTALIUM Linnzus

Subgenus FISSIDENTALIUM Fischer
Dentalium (Fissidentalium) esmeraldum, n. sp. Plate 6) figso ios 2eeno

Shell large, solid and very long, gently curved with a slow
taper; tips missing, but at a diameter of 2 millimeters, its cross-
section is circular; surface sculptured with strong, longitudinal
riblets which are fairly regular in the middle section, become
irregular or alternating towards the tip; near the ventral aper-
ture, the ribs begin to fade out and the surface becomes smooth ;
at a diameter of 7 millimeters, the ribs generally number about
23 and about 14 at a diameter of 3 millimeters; on the earlier
parts of the shell, the ribs are narrow and are separated by very
wide intervals, beautifully etched by the raised lines of growth;
on the mature parts of the shell, 2 or 3 secondary ribs are pres-
ent in the interspaces which increase slowly in size and are
separated from the older set by narrow lines only,

The following measurements are from fragments only.

Length, 61 mm.; diameter, 10 mm.
Length, 60 mm.; diameter, 12 mm.
Length, 39 mm.; diameter, 7.5 mm.

Large Dentalia are common in certain Tertiary formations in
tropical America and in some shale deposits are frequently the
only fossils. Perfect specimens are rare, the apical portion be-
ing invariably lacking so that their identification must be based
largely on size and the surface ornamentation. Most Fissiden-
taliwm are considered deep-water forms.

bo
Ww

BuricA PENINSULA FossiIus: OLSSON 81

Dentalium granac'anum Anderson** from the Las Perdices
shales of northern Colombia and Dentalium uscarianum Olsson**
from the Upper Uscari of Costa Rica are nearest related to
esmeraldum. The Dentaliwm solidissimum Brown and Pilsbry*®
is based on a single fragment from Colombia, the locality not
stated. This species is probably distinct from D. granadanum
with which it was united by Weisbord.*" The primary ribs on the
form, numbering about 28, are narrow and separated by wide
intervals. In D. granadanum, of which I have a good series
from Puerto Colombia, the ornamentation is persistent, the shell
remaining strongly sculptured throughout life while in D. esmeral-
dum, the mature sections of the shell are smooth. From Den-
talium buricum, the Ecuadorian species is distinguished by its
straighter shell, less curved apical portion and fewer ribs.

Type.—Paleontological Research Institution, No. 4069; other
specimens, No. 4070.

Occurrence.—Esmeraldas. formation (upper Oligocene) of
Punta Gorda, Province of Esmeraldas, Ecuador.

Dentalium (Fissidentalium) buricum. n. sp. Plate 6, figs. 3, 4, 5, 6, 9

Shell large, solid, tapering gradually in the lower part, more
rapidly near the tip which is also more strongly curved; tips
missing in our specimens but at a diameter of 2 millimeters or
more, the cross-section is circular; surface is sculptured with
numerous, irregular, low, rounded, longitudinal ribs which fade
out ventrally and are practically missing from the lower part of
mature shells; lines of growth oblique, becoming more crowded
towards the tip where the longitudinal ribs are also separated
by wider or deeper interspaces; at a diameter of about 7 milli-
meters, the longitudinal ribs number about 38 and at a diameter
of 34% millimeters there are about 15 primary ribs and an equal
number of secondary ones.

37 Anderson, F. M.: Proce. California Acad. Sci., 4th series, vol. 18,
1929, p. 144, pl. 13, fig. 3

38 Olsson, A. A.: Bull. Amer. Paleont., vol. 9, 1922, pp. 338, 339, pl.
tio ale

39 Brown, A., and Pilsbry, H. A.: Proe. Acad. Nat. Sci, Phila., vol.
GW), IIE es Si, joule Gy sales fey

40 Weisbord, N. E.: Miocene Mollusca of northern Colombia, Bull.
Amer. Paleont., vol. 14, 1929, p. 26, pl. 5, figs. 10, 11.

82 BULLETIN 106 234

Length, 56 mm.; diameter, 13.5 mm.
Eeneoth, 47> mims, diameter, «10-0. ait:
Length, 45 mm.; diameter, 12.0 mm.

The above measurements are of fragments only but a full-
grown shell would have a length of about 100 millimeters. One
piece in our collection has a diameter of 15 millimeters although
broken off considerably above the ventral aperture.

This species is common in the tuffaceous shales exposed along
the beach on the west side of the Burica Peninsula associated
with Buridrillia panarica. Another large Dentalium, perhaps
allied to this species, occurs in the Pleistocene of Rabo de Puerco
and Monteverde ravines near Puerto Armuelles. These Pleisto-
cene shells are usually badly weathered so that the surface is
chalky but in one specimen the surface is smooth over the greater
part of the shell.

Type.—Paleontological Research Institution, No. 4071; other
specimens, No. 4072.

Occurrence.—Tuffaceous shales, west side of the Burica Pen-
insula, Costa Rica.

PLATES

Plates furnished gratis by the author

PEATE (14)

84 BuLLETIN 106

EXPLANATION OF PLATE I (14)

bo
Cc

Figure Page

1. Placuanomia panamensis, n. sp.
Holotype, interior view; length, 54 mm.
Pleistocene, Rabo de Puerco.
2. Acila isthmica burica, n. subsp.
Paratype; length, 32 mm.
Quebrada Penitas.
. Nuculana (Jupiteria) davidana, n. sp.
Holotype; length, 27 mm.
Charco Azul.
4, Placuanomia panamensis, n. sp. i= ee
Holotype, external view; length, pie mm.; same specimen as
figure 1.

peu)

al

Placuanomia panamensis, n. sp.
Paratype; length, 42 mm.; interior view showing Hee arma-
ture and byssal plug.
Rabo de Puerco.

6. Acila isthmica burica, n. sp. : na.
Holotype, dorsal view; length, 29 mm.
Quebrada Penitas.

Nuculana (Jupiteria) chiriquiana, n. sp.
Holotype; length, 20 mm.

Chareo Azul.

8. Acila isthmica burica, n. sp.
Holotype, same specimen as figure 6.

9. Acila isthmica burica, n. sp. ee See PB es
Paratype, dorsal view; length, 27 mm.

a

Buu. AMER. PALEONT. No. 106, Pu. 1

Pu. 14, VOL. 27

PLATE 2 (15)

86 BULLETIN 106 238
EXPLANATION OF PLATE 2 (15)
Figure Page

i Solemya, (Acharax)) butica, 1.) Spy wel oe

Holoytpe; length of fragment, 58 mm.
Burica sandstones, Burica Point.

2 Calyptogenas panamensis;ni) SD. ea ee 33
Paratype; length, 26 mm.

Burica sandstones, Burica Point.

3. Calyptogena panamensis, n. sp. — — i emeetre em 88}
Holotype; length, 45 mm.

Burica sandstones, Burica Point.

4. Thyasira bisecta Conrad — Lys ee ee 35
Cast of a left valve; length of fragment, 70 mm.

Burica sandstones, Burica Point.

5. Pseudamusium terryi, n. sp. —— Earn reise SY)
Paratype; height, 14 mm.

Chareo Azul.

6; Pseudamusium ‘terryi; n.‘Sp. 222 EEE 30
Holotype; height, 15 mm.; specimen whitened with ammon-
ium chloride.

Chareo Azul.

tj; (2seudamusium: terryi, n; sp... eee eee 30
Same specimen as last, unwhitened.

8 (Corbula) (Varicorbula) ‘cranti, nivsp. 222 eee
Holotype; length, 11.5 mm.

Gharco Azul, 9. -)° SA) fp eee be

925Corbula) (Viaricorbula)) crantijms (sp) 45

Paratype; length, 10.5 mm.
Charco Azul.

Pu. 15, VOL. 27 Buu. AMER. PALEONT. No. 106, Pu. 2

Pea he 2) (16)

240

Page -

66

32

26

40

29

29

88 BULLETIN 106
EXPLANATION OF PLATE 3 (16)
Figure

1. Luciploma panamensis, n. sp. ——
Holotype; height of fragment, 36.5. mm.
Burica sandstones, Burica Point.

2. Luciploma panamensis, n. sp. —-
Same specimen as last to hor saanion,

3. Hanetia pelicana, n. sp. ——
Holotype; height, 38 mm.
Burica sandstones, Burica Point.

4. Periploma lucina, n. sp. :
Holotype; loneune 38.5 mm.
Rio Guanabanon.

5. Voldia; (Orthoyoldia)) quiba, ns). 2 eee
Holotype; length, 27 mm.
Chareco Azul.

6: Chione: (Chione)araneosa; n. sp. Se eae
Holotype; length, 33 mm.
Burica sandstones, Burica Point.

7. Areca (Scapharca) charcoazulensis, n. sp. —
Holotype; length, 35 mm.
Chareco Azul.

8. Arca (Scapharea) charcoazulensis, n. sp.
Paratype; length, 33 mm.
Chareo Azul.

9. Condylocardia panamensis, n. sp.

10.

Holotype; length, 1.75 mm.
Punta de Piedra.

Condylocardia panamensis, n. sp. ——...- ESSERE

Paratype, internal view.
Punta de Piedra.

Buu. AMER. PALEONT. No. 106, PL. 3

Pu. 16, VOL. 27

REAGE, 4 C17)

90) BULLETIN 106 242

EXPLANATION OF PLATE 4 (17)

Figure Page

1. Lucina (Lucinoma) chiripanica, n. sp. J eoectee de
Holotype; length, 54 mm,
Charco Azul.
Nucula iphigenia azulensis, n. subsp. —.. et eres se Se
Paratype; length, 30.56 mm.
Charco Azul.
3. Tellina (Macaliopsis) frontera, n. sp. Pee 42
Holotype; length, 44 mm.
Quebrada Penitas.

bo

4. Lucina (Lucinoma) chiripanica, n. sp. oe Sesto csc
Paratype; length, 35 mm.
Chareco Azul.

5. Nuculasiphigenta azulensis. ne subspy eee JES:
Holotype; length, 35 mm.
Chareo Azul.

6; ellinay(Macaliopsis)) )2rontexay crise iS ey cee 42
Holotype; same specimen as fig. 3.

(miNuculasiphigenta azulensiss) ns SubSpy coe 24

Paratype; length, 30 mm.
Chareo Azul.
8. Macoma (Macoploma) medioamerciana, n. sp. eee CY!
Holotype; length, 62 mm.
Quebrada Penitas.

Pu. 17, Vou. 27 Buuu. AMER. PALEONT. No. 106, Pu. 4

PLATE 5 (18)

96 BULLETIN 106 248
EXPLANATION OF PLATE 5 (18)
Figure Page

i Pitar (luamelliconcha) anona, 1. sp3 37
Holotype; length, 35.5 mm.
Rio Guanabanon.

o-= Macrocallista, tratton! 2. sp3 EE 38
Holotype; length, 33 mm.
Rabo de Puerco.

3. Macrocallista traftoni, n. sp. sts Hige Mine remem iti es 38
Paratype; length, 29 mm.
Rabo de Puerco.

4. Pitar (Lamelliconcha) mellisa, n. sp. =. eee ot
Holotype; length, 47 mm.
Quebrada Mellisa.

5. Macoma (Panacoma) chiriquiensis, n. sp. —...--------_- 43
Holotype; length, 34 mm.
Charco Azul.

6. Macoma (Panacoma) chiriquiensis, n. sp. 43
Paratype; length, 37 mm.
Chareo Azul.

i. (Chione! (Chione)* vaca, n. sp. 2 ee eee 40
Holotype; length, 27.5 mm.
Rio La Vaea.

8. Sanguinolaria (Sanguinolaria) azulensis, n. sp. 42

Holotype; length, 35.5 mm.
Charco Azul.

PL. 18, VOL. 27 Buu. AMER. PALEONT. No. 106, Pu. 5

PLATE 6 (10)

Ob

BULLETIN 106

EXPLANATION OF PLATE 6 (19)

Figure

1

10.

Hal

12.

13.

Dentalium (Fissidentalium) esmeraldum, n. sp... -----

Paratype; length, 60 mm.
Punta Gorda, Ecuador.

. Dentalium (Fissidentalium) esmeraldum, n. sp.

Paratype; length, 39 mm.
Punta Gorda, Ecuador.

Dentalium (Fissidentalium) buricum, n. sp.
Paratype; length, 44 mm.
West side of Burica Peninsula.

. Dentalium (Fissidentalium) buricum, n. sp.

Holotype; length, 57 mm.
West side of Burica Peninsula.

. Dentalium (Fissidentalium) buricum, n. sp. -

Length, 61 mm.
Rabo de Puerco.

. Dentalium (Fissidentalium) buricum, n. sp.

Paratype; length, 48 mm.
West side of Burica Peninsula.

Ringicula (Ringiculella) costaricensis, n. sp.
Holotype; length, 2.6 mm.
Quebrada Penitas.

Ringicula (Ringiculella) costaricensis, n. sp.
Paratype; length, 2.6 mm.
Quebrada Penitas.

. Dentalium (Fissidentalium) buricum, n. sp.

Paratype; length, 44 mm.
West side of Burica Peninsula.

Dentalium (Fissidentalium) esmeraldum, n. sp.
Holotype; length, 61.5 mm.
Punta Gorda, Ecuador.

Conus (Leptoconus) arcuatus vacuanus, n. subsp.
Holotype; height, 46 mm.
Quebrada Mellisa.

Conus (Leptoconus) arcuatus vacuanus, n. subsp.

Paratype; height, 36 mm.

Quebrada Mellisa.
Conus arcuatus Sowerby

Height, 39 mm.

Rio Guanabanon.

246

Page
80

80

81

81

81

81

19

795

81

80

49

49

Buu. AMER. PALEONT. No. 106, Pu. 6

PL. 19, VoL. 27

RieAwie7) (20)

92

BULLETIN 106

EXPLANATION OF PLATE 7 (20)

Figure

ol

. Clathrodrillia (Buridrillia) panarica, n. sp.

. Clathrodrillia (Buridrillia) panarica, n. sp. -

Holotype; length, 50 mm.
Quebrada Penitas.

Holotype; length, 62 mm.
Chareo Azul.

) Lurricula dulcia; n:) spe ===

Holotype; length, 47 mm.
Quebrada Penitas.

. Clathrodrillia (Buridrillia) panarica, n. sp. ~~~

Holotype; length, 72 mm.
Chareo Azul.

Paratype; length, 51 mm.
Chareo Azul.

. Turricula dulcia, n. sp... Ses eee ad ee

Paratype; length, 41 mm.
Quebrada Penitas.

Paratype; length, 54 mm.

Tuffaceous shales, west side of Burica Peninsula.
. Turricula (Knefastia) andesita, n. sp. —\

Holotype; length, 46 mm.
Mouth of Quebrada Penitas.

'Rusiturricula’ woodringi ns) Sn

244

53

54

52

oO
or

Pu. 20, Vou. 27 BULL. AMER. PALEONT. No. 106, Pu. 7

PLATE 31)

OS

Figure

il,

10.

BULLETIN 106

EXPLANATION OF PLATE 8 (21)

Cancellaria (Charcolleria) terryi, nm. )sp-e
Holotype; length, 41 mm.
Quebrada Penitas.

i Nassa. (Uzita) terryi, ns Sp. ee eee eee

Holotype; length, 23 mm.
Charco Azul.

. Cancellaria (Bivetopsis) charapota, n. sp. 2 de

Holotype; length, 22 mm.
Charapota, Ecuador.

. Cancellaria (Cancellaria) penita, n. sp. — — ——eesSsSsSFSFSSFSs

Holotype; length, 27 mm.
Quebrada Penitas.

. Cancellaria (Charcolleria) perdiciana, n. sp.

Holotype; length, 60 mm.
Puerto Colombia, Colombia.

. Nassa (Uzita) armuella, n. sp. ees st

Holotype; length, 21 mm.
Chareo Azul.

2 Nassa.CUzita)Ntertyiy on. Spy i = ee eee eee

Paratype; length, 20.5 mm. :
Chareo Azul.

. Cancellaria (Cancellaria) penita, n. sp. oles hts CES eee ee ere

Paratype; length, 25 mm.
Quebrada Penitas.

. Nassa (Uzita) terryi, n. sp. badge pen te a

Paratype; length, 18.5 mm.
Charco Azul.
Latirus:penituis;,: ne) Spi) 22 a eee ss
Holotype; length, 53 mm.
Quebrada Penitas.

250

60

59

61

ral

59

70

64

Bun. AMER. PALEONT. No. 106, Px. 8

Pu. 21, VOL. 27

PEATE: (22)

100

BULLETIN 106

EXPLANATION OF PLATE 9 (22)

Figure

1.

6.

10.

Cymatophos panamensis, n. sp.
Holotype; length, 44 mm.
Rio La Vaca.

Dalium ecuadoriana, n. sp.
Paratype; height, 39 mm.
Punta Gorda, Ecuador.

Dalium ecuadoriana, n. sp.
Holotype; height, 43 mm.
Punta Gorda, Ecuador.

Cancellaria colombiana, n. sp.
Holotype; height, 33.5 mm.

Las Perdices shales, Puerto Colombia, Colombia.

Phos (Antillophos) rutschi, n. sp.
Holotype; height, 30 mm.
Quebrada Penitas.

Epitonium (Ferminoscala) ferminianum Dall
Height, 41 mm.
Charco Azul.

Fusinus mellisus, n. sp.

Holotype; height, 82 ane
Quebrada Mellisa.

. Metula pilsbryi, n. sp.

Holotype; height, mB mm.
Rio La Vaca.

. Metula amosi Vanatta

Height, 44 mm.

Pleistocene, Thatcher’s Ferry, Canal Zone.
Clathrodrillia harrisi, n. sp. —

Holotype; height, 32.5 mm.

Quebrada Pejnitas.

252

Page:
yal

4
4

ele it

73

69

Pu. 22, VOL. 27 Buu. AMER. PALEONT. No. 106, Pu. 9

PEAT Bron (23)

102 BULLETIN 106 254
EXPLANATION OF PLATE I0 (23)
Figure Page

1. Hanetia (Fusinosteira) alternata Nelson —_----...._ 67
Length, 70 mm.
Chareo Azul.

2. Natica (Natica) scethra burica, 1. subsp) EE 79
Holotype; length, 27.5 mm.
Chareo Azul.

3. Strombina fusiformis penita, n. subsp, ~~. eee 74
Paratype; length, 34 mm.
Quebrada Penitas.

4. Ancistrosyrinx cedonulli reevei, n. subsp. = sé=<Cs«~iS “SB
Holotype; length, 43 mm.
Chareo Azul.

5. Strombina (Cotonopsis) panacostaricensis, n. sp. — ~~~ 75
Holoytpe; length, 32 mm.
West side of Burica Peninsula.

6. Strombina fusiformis penita, n. subsp. 74
Holotype; length, 34.5 mm.
Quebrada Penitas.

f@ Naticascethrasburica, n- subsp. ee
Charco Azul.

8. Strombina fusiformis penita, n. subsp... 74
Paratype; length, 26 mm.
Quebrada Penitas.

9. Mitrella (Longitrella) vespertina, n. sp. | Ss 73
Holotype; length, 25 mm.
Charco Azul.

10. Pleurotomella (Phymorphynchus) agina, n. sp. 56

Holotype; length, 27.50 mm.
Charco Azul.

No. 106, Pu. 10

Buuu. AMER. PALEONT.

Pu. 23, VOL. 27

PLATE rii(24))

104

BULLETIN 106 256

EXPLANATION OF PLATE I1 (24)

Figure Page

iL

bo

10.

. Terebra (Strioterebrum) cracilenta Li

. Terebra (Strioterebrum) vaca, n. sp.

. Clathrodrillia harrisi, n. sp.

Cantharus amycus, n. Sp. —-—-----—---—-------------—------ DGS
Holotype; length, 44 mm.
Burica sandstones, Burica Point.

. Hanetia anomala burica, n. sp. ——----—-------- Jo jee 67

Holotype; length, 49 mm.
Quebrada Mellisa.

. Terebra (Strioterebrum) panamillata, n. sp. —-—--.-- Sh: Se 48

Holotype; length, 32 mm.
Rabo de Puerco.

. Terebra (Strioterebrum) guanabana, n. sp. ~~~. 46

Holotype; length, 69 mm.
Rio Guanabanon.

Length, 38.50 mm.
Rio La Vaca.

Terebra (Strioterebrum) vaca, n. sp. —--------______- Aa ae 47
Holoytpe; length, 42 mm.
Rio La Vaca.

Same specimen as figure 6.

Paratype; length, 34 rae
Quebrada Penitas.

Cancellaria (Calearata) peninsularis, n. sp. ~~... 62
Holotype; length, 31 mm.
Quebrada Penitas.

Alvania bartschi, n. sp. - oe nn

Holotype; length, 1.25 mm.
Punta de Piedra.

BuLu. AMER. PALEONT. INO, IMOKa, Jeie, Jl

Pu. 24, VOL. 27

ALND > (215)

106

BULLETIN 106

EXPLANATION OF PLATE

Figure

le

Or

6.

=|

Borsonia (Borsonella) adamsi, n. sp. ——

Holotype; length, 27 mm.
Chareo Azul.

. Leucosyrinx nicoya, n. sp.

Holotype; length, 21 mm.
Chareo Azul.

?Leucosyrinx buricana, n. sp.
Holotype; length, 38 mm.
Chareo Azul.

. Polystira panamensis, n. sp. ~~~

Holotype; length, 23 mm.
Chareo Azul.

. Typhis (Talityphis) costaricensis, n. sp.

Holotype; length, 22 mm.
Quebrada Penitas.

Borsonia (Borsonella) harrisi, n. sp.
Holotype; length, 15 mm.
Chareco Azul.

Borsonia (Borsonella) harrisi, n. sp. -
Paratype; length, 14.75 mm.
Chareo Azul.

12)(25))

Typhis (Talityphis) costaricensis, n. sp. -

Holotype; same specimen as figure 5.

258

Page
58

57

52

76

59

59

76

No. 106, Pu. 12

Buu. AMER. PALEONT.

PL. 25, Vou. 27

ne ‘ mn or
ois

4

-- PaLEonroLocicaL REsEarcH INSTITUTION ~~

Ithaca, New York -

Volume bk (Nos. 158), 854 pp. 32 ae ee
z= Mainly Tertiary Mollusca, ; ;
if. (Nos. ee 347 pp, 23 pis.

Ses eS ~ faunas. = : a tio
Sts PIV: (Nos. 16-21). 161 pp., 26 pls. ee eae eats

s Mainly Tertiary Mollusca and sections of Pa
ee tions and faunas.

V. (Nos. 22-30). > 437 pp. 68 pls. =

-. Tertiary fossils mainly Santo Domingan, Mesozoic and
ansaid Paleozoic fossils, ; Ga aR =e
“8 < VE. (No. S1).-) 268, 59 pls. 4/5 poses Ss (

~ Claibornian Hocene melcurpode ine fu

VIL. (No. 32). 780 pp., 90 pee a 6

pods,

VAIL. (Nos. 33-36). 357 pp., 15 ae 7
= Mainly Tertiary Mollusca. _ hes
. (Nos. 37-39). 462 pp., 35 pls. ReNeAS Se aa e fae Bs ae

‘Tertiary Mollusca mainly from oe Rica. ms a
Xx. (Nos. 40- 42), S82. Dp. D4 pis. ee

Paleozoic fossils. <3 eS =

Kl. Néd: 48-46); G7 pprodl ple a ss 2 Se ae
Tertiary, Mesozoic and Paleozoic fossils. “mainly” from
Venezuela. es Sate

XI (Noss 47-48) 249¢ pos 8 pla ge Se
¢ : - Venezuela and Trinidad Params and Mesozoic inverte-

2 Sh . -brate bibliography. = : tin.

~ “xa. (Nos.849-50) 2264 ppt piss tos ee ee

{ Venezuelan Tertiary Mollusca and Tertiary Mamma

"XIV. (Nos. 51-54) -> 306" pity a Spl sr ek

ss - _ Mexican Tertiary forams and Henlasy mollusks a e
and Colombia. eh

~ “Complete titles and price jist of all numbers Miprites had oni
_ tion. All volumes available.

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 107

A Median Dorsal Plate of Holonema
from the Upper Devonian of New York

By

John W. Wells

February 1, 1943

Paleontological Research Institution
Ithaca, New York
WigreHes

of Compas>
KP" rocions ie
FEB 9 1948

LIBRARY

13,9b/

A MEDIAN DORSAL PLATE OF HOLONEMA FROM
THE UPPER DEVONIAN OF NEW YORK
By
Joun W. WELLS

The Ohio State University

INTRODUCTION

Recently I described a large median dorsal plate’ from the
Enfield formation (Naplesian) of central New York (1924). It
was identified with a ventral plate, originally described as Glyp-
taspis abbreviata by Eastman (1907, p. 147, pl. 13), and placed
in a new genus, Deirosteus, of the arthrodiran family Holonemi-
de (rect. Holonematide). At that time the only certain distinc-
tion between this new form and Holonema. Newberry was the
surface ornamentation of the plates. Now, through the fortunate
discovery of a small but nearly complete example of the median
dorsal plate of Holonema rugosum (Claypole)—one of the many
heretofore unknown plates of this curious fish?—direct compari-
son can be made between two corresponding parts of Deirosteus
and Holonema. This comparison, as will be shown, serves to
confirm my separation of the two genera.

I am under obligation to Dr. K. V. W. Palmer, who noted the
specimen in the geological collections at Cornell University and
recognized its significance, and to the Department of Geology of
Cornell University which has generously defrayed the cost of the
illustrative plate. Credit for the discovery (in 1940) of the speci-
men is due Mr. G. E. Bentley of Jamestown, N. Y., who kindly .
donated it to Cornell.

1 Pal. Res. Inst. Cat. No. 5945.

2 The hinder portion of an MD of H. rugosum was collected several
years ago from the Oneonta formation in Chenango County, N. Y., but
only the interior surface with the posterior process can be discerned,

4 BULLETIN 107 262

LOCALITY AND HORIZON

The specimen is an external mold on the surface of an irregu-
lar block of thoroughly leached sandstone packed with molds of
invertebrates. It was found as float in a field a mile east of the
village of Maine, in western Broome County, southern New York.
The bedrock in this area, according to the Watkins Glen Cata-
tonk atlas map (1909), is near the lower (paleontologic) bound-
ary of the Chemung formation, but the specimen may be erratic,
derived from a lower formation, probably the next older, the En-
field. The lithology is that of the Chemung, but in this area
Chemung lithology extends below the base of that formation into
the Enfield. The only recognizable significant invertebrate fossil
in the block is Spirifer mesacostalis which suggests either a Che-
mung horizon or the Enfield not far below the base of the
Chemung.

This association of a plate of Holonema with a marine inverte-
brate assemblage does not necessarily imply a marine life environ-
ment for this fish, for its remains are more commonly found in
continental deposits indicative of fresh-water environments, not
only in this country but in Russia (Obruchew, 1933, p. 113) and
Spitsbergen (Heintz, 1935).

Genus HOLONEMA Newberry
Holonema rugosum (Claypole) Plate 1
Description of the MD

The median dorsal plate (Cornell Univ. Geol. Coll., No. 38706)
is represented by an external mold which is complete posteriorly
but lacks about one-fourth of the anterior end. The left side of
the fore part also is missing. Compared with other known plates
of H. rugosum, such as the ventral shield, it represents a rather
small individual, probably less than half size.

Dimensions.—Length (preserved) T4.

7

Length (estimated original®) 1

’ This length is arrived at on the assumption that the center of. ossifi-

cation lies about four-fifths of the distance from the anterior to the pos-
terior end, as in most arthrodires.

5]

DEVONIAN HoLONEMA: WELLS

bo
a
(Sh)

Maximum width (at center of

ossification ) 7.9
Width at posterior end 5-4
Maximum convexity (anteriorly) I

Outline elongate-rectangular, narrow, proportions about 2.3:1,
convex anteriorly, nearly flat behind the center of ossification.
Sides nearly straight, gently tapering forwards, with a_ slight
reentrant anteriorly and a strong one posteriorly and a strong
bulge opposite the center of ossification, Posterior corners trun-
cated; posterior margin slightly convex.

External ornamentation, in general plan, like that of Deirosteus
abbreviatus (vide Wells, 1942, p. 652, pl. 95), in five zones: a
central “club”, a lateral and posterior concentric broad ridge and
narrow interspace system, a lateral and posterior submarginal
reticulate area, a marginal zone of parallel ridges at right angles
to the margin, and a fan-shaped antero-central reticulated zone.

A sensory canal groove on either side of the central “club”
about two-thirds of the distance from the anterior to the posterior
end, commencing at the inner edge of the marginal zone of par-
allel ridges, curving backwards across the submarginal reticulate
zone and well into the central concentric ridge system, but not
extending back so far as the center of ossification nor joining
across the middle.

DISCUSSION

Comparison of the figure of this MD of H. rugosum with that
of Deirosteus abbreviatus, previously cited, reveals very close
similarity in general shape and in the surface sculpture plan,
and at the same time indicates two outstanding differences be-
tween the two genera: the difference in detail of sculpture and
presence of sensory canals in the former. In Deirosteus, the cen-
tral sculpture consists of narrow ridges with broad tuberculated
interspaces ; in Holonema, the ridges are at least equal to, and
usually broader than the interspaces. In Deirosteus, the mar-
ginal sculpture consists of rows of fine granulations ; in Holonema,

6 BULLETIN 107 264

of parallel ridges. No sensory canals occur on the MD of
Deirosteus, and this is perhaps a more significant generic distine-
tion than that based upon ornamentation. Their curvature is
contrary to that of the same canals on MD’s of most arthrodirans
which are curved backwards rather than forwards, but is the
same as that of the canals on the MD of another holonematid,
Megaloplax marginalis (Eichwald) (Obruchew, 1933, pl. 7; fig:
2) from the lower Upper Devonian of Russia.

The MD of the other fairly well-known species of Holonema,
H. radiatum Obruchew (1933, p. 100), from the lower Upper
Devonian of Russia, has been described (ibid, p. 103). It corre-
sponds very closely in shape (especially posteriorly) and orna-
mentation with the new MD, except that no sensory canals have
been noted, The condition of preservation of the external sur-
face of the Russian plate, however, is bad and they may not have
been preserved. ‘The MD of H. radiatum is proportionally
longer (2.6:1 compared with 2.3:1), suggesting that H. rugosum
was a somewhat plumper fish.

Only two species of Holonema are at present even moderately
well known‘: the genotype, H. rugosum of the Naplesian and
Chemungian of New York and Pennsylvania (and apparently the
Erian of Michigan and Wisconsin), and H. radiatum of the
lower Upper Devonian of Russia and Spitsbergen. Previously
I suggestedl (1942, p. 654, pl. 97, fig. 4) that the Holonema plates
described from the Traverse series of Michigan by Case (1931,
p. 173, pl. 4, figs. 1, 2) indicated a new species, but further study
of the Michigan Devonian specimens and specimens of undoubt-
ed H. rugosum from the Upper Devonian of New York does not
yield any criteria for species discrimination. The ornamentation
is the same and the only plates known in common between the
two, the right externo-basals, are exactly the same, even to their

4 Others, known from more or less imperfect fragments, are: H. hor-

ridum Cope (Chemungian, Pennsylvania), H. ornatum Traquair (Upper
Devonian, Great Britain), and H. eifeliense (Kayser) (Middle Devonian,
Germany). Neither of the last two belongs to Holonema and H. ornatum
is probably not an holonematid.

~~

HoLONEMA: WELLS

DEVONIAN

265

3/TX {VS ‘oO ‘uetuoaog sasddg pue ofppryy ‘(epodéelp) wnsoins Wg

‘ot/ex ‘ (Eg6T ‘moyoniqo
woIz peytpoyw) ‘eissny ‘ueruoasq szeddq ‘moyonaqg wnynipp.s “A “VW
‘DwWauo)0
FO Spperys [erueso Fo yavd pue [esdop Fo yoodse [esiop JO WoTpoNI}SUOdIy

V
g

8 BULLETIN 107 266

dimensions. Fragments of the antero-dorso-lateral are known
from both areas, but not of the same parts of the plates. For the
present, then, H. rugosum appears to range from the Middle
(Erian) well into the Upper (Chemungian) Devonian.

It may be premature to attempt reconstruction of the plan of
the cuirass of this fish, but I believe I am taking no great liber-
ties in presenting the tentative sketch shown in the text figure
(B), wherein Obruchew’s plan of H. radiatum, redrawn and
slightly modified, has been used as a guide. The plan of H.
rugosum is based upon the MD just described and upon others
(EB, MB, ADL) from the Oneonta (Naplesian) formation of
Chenango County, N. Y., and upon Case’s material (EB, MB,
ADL) from the Traverse (Erian) series of Michigan (Univ.
Mich. Coll. Nos. 13040, 13043).

REFERENCES
Case, E. C.
Arthrodiran remains from the Devonian of Michigan, Contr.
Mus. Paleont., Univ. Mich., 3, 1931, pp. 163-182, 5 pls., 13 figs.
Eastman, C. A.
Devonie fishes of the New York formations, New York State
Mus., Mem., 10, 1907, 235 pp., 15 pls., 35 figs.
Heintz, A.
Holonema-Reste aus dem Devon Spitzbergens, Norsk geol.
Tids., 15, 1935, pp. 115-121, 1 pl.
Obruchew, D.
Holonemide des russischen Devons, Acad. Sei. U. 8. S. R,,
Inst. Paléozool., Trav. 2, 1933, pp. 97-115, pls. 5-8, 27 figs.
Wells, J. W.
Arthrodiran fish plates from the Enfield formation (Upper
Devonian of New York), Jour. Paleont., 16, 1942, pp. 651-656,
pls. 95-97.
Williams, H. S., Tarr, R. S., and Kindle, E. M.

Watkins Glen-Catatonk Folio, U. S. Geol. Surv., Geol. Atlas,
1909, Folio 169.

PLATES

PLATE 1 (26)

10 BULLETIN 107 268

EXPLANATION OF PLATE I (26)

Figure Page

1) Holonema ruzosum (Claypole)) ee
From the upper Enfield (?) formation near Maine, Broome
County, N. Y. External surface of a nearly complete median
dorsal plate (rubber cast), Cornell Univ. Geol. Coll., No.
38766. Natural size.

No. 107, Pu. 1

Buu. AMER. PALEONT.

Pu. 26, Vou. 27

eS

=> =

n and Mexican Tertiary — i
forams: and lee and Paleozoic ee .
nse: 59-61), Tapp. de pise. ou sok

EES Venezuela and ‘Trinidad ‘Tertiary TWoitiaex
~ xVE. “Wos. 62-63)... 283 - pp 33 “piss
Faget Re Peruvian Tertiary Mollusca. ~~ 2x eats ee
“i XVII. (Nos, GEG) ebeii, 29bis. et rr
_ Mainly Tertiary Mollusca mpd Cretaceous eorals: se)
ee. Sees XIX. (No. 68). 272 pp., 24 pls. Rebels es Ses n
Tertiary Paleontology, ees . es = es
XX. (Nos. 69-70C). 266 pp., 26 BGs ae aes oe ae ee as
Ras: Cretaceous and Pertiary Faleantelosy of. Peru and Cuba,
Roe 230 (Nos. WALT2). API app oie plea Gs ei etiw A
pe Paleozoic Paleontology and Stratigraphy. Festi Feb
XK. Wos. WarT6}s soe. Up.sh piss wee ea oo ge ae a
Soe a leozoic Paleontology and Tertiary Serer baie

= ax: (Nos. 77-79). 251 pps Bp |S, eee
ee Goraise Cretaceous ‘microfauna and biography « of Conrad. ae

~ XXIV. (Nes: BH-S7 oho84 np. Pr pis. 2 ee eee aaa |

ears Mainly Paleozoic faunas “and Tertiary. Mollusca, Sie

(Nos. 88-948), 306 pp., “80 “ite,s=s ee aerser)
aaa - Paleozoic | fossils of Ontario, Oklahoma: ail Colombia,
ae “Mesozoic echinoids, California yseecene and pbk Sy 38
Fe Miocene mollusks. ~ s

(Nos. 9 95- 100). 420 pp., 58 aia OBI oe tee ele ta oe
re _ Florida Recent marine shells, Texas Cretaceous fossils,
yee - Cuban and Peruvian Cretaceous, - and Peruvian Eogene x
; oe corals, and geology and paleontology of Ecuador. Sey ee eee
-XXVIL. (Nos. 101-105, other numbers in preparation.) 152 pp., 13 pls. 3. 25°
ERE tena San Pedro, California Pleistocene Mollusca, type fossil a
SE - Cypreide of North America and early Palezoic cepha- —

Pe eens from Alaska, Kentucky and New ‘York. State.

<

- PALAZON TO GRAPHICA AMERICANA ~ a :

= iS ‘Volume I. (Nos. 1-5): b19pp.:tp- pla. Be eg ee ae gl $12.0 00.
Monographs of arcas, Lutetia, rudistids and Seneca = z

Ti. (Nos. 6- 12). bal pp., 37 pis: Cor IS oe Ee a ae epee
— ae _Heliophyllum halli, Tertiary turrid illustrations, Neo--
saa ecene Spondyli, Paleozoic cephalopods, Tertiary
ss _ Fasciolarias and Paleozoic and Recent Hexactinel-
- lida. ;

Volume Til. “os. 13- 14, other ise 3 in Re prep geataing) 90 pp., 5 pls. 2. 25 Ke
__ Eurysiphonate cephalopod structure and phylogeny and —
Paleozoic siphonophores._

U

BULLETINS

Pee PENG,
Los 0 “DIN way
fe Fe

OF APR

te

3

Zona gS

1943

I ki nS Pe
—_

AMERICAN

PALEONTOLOGY

VOL. XXVII

eS Sevens Sete eee “

NOM BE re 1s

PALEONTOLOGICAL RESEARCH INSTITUTION
Ithaca, New York
GSAS

ra >
#
z
;
f

BULLETINS OF AMERICAN PALEONTOLOGY , Vol. 27, No

FRONTISPIECE

TS 7o°
SE.
B E A N Feta ARUBA
R “a : Ke
c> (ac
LS Gay
owe res GOLFO
B :
fs Vi VENEZ eee
BARRANQUILLA 9 Ww s
" N77 iy
Qric A
. \
Ri Geanacaiso a Ry
RIO GS” < 2o
g bay i Ve ns
5 y* 2 iN F570 Ma EG - #
SS (% <| < J LAGO 10"
re oT a ao DE
: & (MARACAIBO pi
N R re | SS Bie Moe ne 3
=
2 OF
ey cs Oxmy (ohh ta¢ymbe Sa
ay ‘a Nae
Hen MERIDA —
ra ge a
he SS <q»
&/ SS we 4»
Ne Q Wi TACHIRA aN
Qs [ wv
iy s | he
2 2 WQ&«:
ie N NES
‘S) i ‘@) a bante
C) g :
Sars) es > v \ Rie Arauca aoe
& &. & a
yy ~
af a SQ &y © :
< ee,
ae eer)
Qs SANTA ROSA &
© Re or SOGAMOSA
©) wv
w\
Ce) rt 2 a8 aS. ice MILE’
a ioe e ee Ba 190 ee KILOMETERS 70
‘S)
{O. 108, 1943

”~

BULLETINS
OF

AMERICAN PALEONTOLOGY

Vol. 27

No. 108

The Rio Cachiri Section in the

Sierra de Perija, Venezuela

R. A. Liddle, G. D. Harris and

J. W. Wells

Aprtl\6 \ 1943

Paleontological Research Institution
Ithaca, New York
WSs ay

ei com
.;) Br.
KE zoology

[® e'
(apm 13 14943 )

LiBRAK

inqb|

CONTENTS

Location and accessibility
Introduction
Acknowledgments - : :
Stratigraphy PAN ey ee
Tgneous rocks : =~ ix cn een
Acidic group - ee Pee ge ee
Basic group
Metamorphic rocks astra
Pre-Devonian: probably ARanaaaie ae
Sierra de Perija series

Namie: =: Bo eee ee ae Se a PED

Stratigraphic. Dosen
Physical character
Extent and thickness -
Age and correlation

Topographic expression ad local igen

Sedimentary rocks ene as
Paleozoic So ee a

Lower and Middle Devoe Rie Cacia series

Cano Grande formation
Names ==

Str atieraphic positon

Physicals character. === ae = ‘i E ha: — ant hae 2

Extent and thickness
Age and correlation —_

Topographic expression Bie Tgeeil set enily

Upper. Devontan === as te

Cano del Oeste formation —

IN ane: pen ae oe ae ee ee
Siar eenenlne” nosnar

IPA SMOAI, “Clieneieyere ee

Eeabenitnsanid sthickwniescu ee a Ss ek

Age and correlation

Topographic expression and Moca details

Campo Chico formation
Name

Stratieraphic! Rest saa.

Physical character: ==
Extent and thickness
Age and correlation

Topographic expression eh local Gees es

Devonian—Permo-Carboniferous relationship
Permo-Carboniferous

Palmarito series ____ Ne ER oe a
Namie. == a ey eS ee
Stratigraphic ‘position Sc sake eS Se ee ee
ies SiiGeUlam OM aa CLC Wee eas LN ee

Hxtentmand thickness =. :
Acemande correlabione 22" = = =e
Topographic expression and local details

Permo-Carboniferous—Cretaceous relationship
Mesozoic eee an: hone

Lower Cretaceous :
Rio Negro formation

IN anne) saa es a See ee ee ee

Stratigraphic sesheiom enews

Physical character

Extent and thickness

Age and correlation —

Topographic expression Pea last details

Corolllowskormaclony pees ee eee

Namie) = 2 es Ey eee
Stratigraphic position
Physical character

Extent and thickness

Age and correlation —— —__

Topographic expression and local Pacis)

Middle Cretaceous: <Guayaiitaseono up

Guayuta shale

La Luna formation —

Name Pie Mates tie twirl 5
Stratigraphic “position

Physical character

Extent and thickness _

Age and correlation ——___

Topographic expression Bad iipeal derales

Name) =e = eet pan ee, & SET eee eee a a

Stratigraphic aaehihion pe arees “ee ees
Physical character ___ see

Extent and thickness —__

Age and correlation

Topographic expression and local details

The Cretaceous-Eocene relationship _...- = eee

Cenozoic

Lower Eocene __

Rio Guasare formation | ee ee
INIQING) toe ee ed ee ee

Stratigraphic position

Physical character -... ae re Nea RE SED
Extent and thickness Peet ok
Age and correlation

Topographic expression and ie details —_
Misoa-Trujillo formation: Third Coal horizon

Name —__ ee eee ae a!
Stratigraphic position
Physical character
Extent and thickness |
Age and correlation —_____

Topographic expression and local details

Structural geology =

Description of samples from Bick Cachirt -
Samples from the Cano del Norte branch of Rio Cachiri
Samples from the Cano del Oeste branch of Rio Cachiri
Samples from the Cano Grande branch of Rio Cachiri

Plates
Maps

Opposite

Fr ontispiece and opposite

29
29

32

34

36

47
54
54

THE RIO CACHIRI SECTION IN THE
SIERRA DE PERIJA, VENEZUELA
PART TI. GEOLOGY

By

2

R. A. LIDDLE

LOCATION AND. ACCESSIBILITY

Rio Cachiri rises in the-high, cloud-capped mountains of the
Sierra de Perija along the boundary between Venezuela and
Colombia. It flows northeastward to join Rio Socuy in forming
Rio Limén whose waters reach the Gulf of Maracaibo, an arm
of the Caribbean Sea, through Lago Sinamaica. The first 20
kilometers of its course are amid wild, rugged, forest-clad peaks
from which it descends over falls, down boulder-choked gorges
and narrow, densely forested valleys until it breaks through the
frontal barrier at the eastern edge of the range to meander north-
eastward across semiarid lowlands.

West of the frontal barrier there are no human habitations, and
few people have undertaken the arduous climb to the upper
reaches of the river because all food, with the exception of meat,
and equipment must be carried by man. Furthermore, the ascent
may be made only near the end of the dry season, during the last
half of February and the first half of March, when the river is
at its lowest stage, for the river bed affords the only way of access.
Even at the end of the dry season trails must be cut around some
gorges and falls like those just west of Playa La India where the
river has worn a narrow, vertical-walled canyon through sand-
stone and shale of the Misoa-Trujillo formation of lower and
middle Eocene age that makes up the frontal barrier ridge of the
mountains. Where the river cuts through soft shale no gorges
or waterfalls are found but the stream bed is difficult to traverse
because it is choked by fallen trees interlaced with vines.

6 BULLETIN 108 274

Playa La India may be reached by mule in one day from
Rancho Rio Viejo farther down on the east bank of Rio Cachiri.
In the dry season Rancho Rio Viejo is accessible from Maracaibo,
with difficulty, by automobile in about five hours.

From Playa La India to Campo Las Tres Bocas game is plen-
tiful. Around the playa, are havolina, danta, paujil, and pavo.
Farther west the amount and variety of game diminish and above
Campo Las Dos Bocas even pawjil and pava disappear, only par-
rots and monkeys being found. In the mountains where the river
is clear and cold a species of vegetable-eating fish called boca
chica is abundant but it does not take a lure. As pools in the
river are fairly shallow at the end of the dry season a seine can
be used effectively. The fish travel in schools of 200 to 500 and
weigh uniformly from one and one-half to two pounds each.

INTRODUCTION

In the early part of 1924 C. W. Yeakel, P. W. McFarland, and
R. A. Liddle traversed Rio Cachiri from its mouth westward into
the Sierra de Perija almost to the source of its north fork, now
referred to as Cano del Norte. Fossils were collected from the
Eocene, the Cretaceous, the “Old Red series” which was provi-
sionally placed in the Permian, and from the Lower and Middle
Devonian. Some of this Devonian fauna was described by
Weisbord’, and some of it was listed by Liddle’.

In 1926 Joe Netick, G. A. Weaver, and Malcom Madera made
a plane-table survey and systematic collec ‘ons of fossils and rock
samples westward from Rancho Cachiri 11to the Devonian sec-
tion on the Cano del Norte and Cano de! Oeste branches of Rio
Cachiri. They did not, however, examine Cano Grande, the
main branch of the river beyond Campo Las Tres Bocas.

In later years a few expeditions up Rio Cachiri have been re-
ported but no one has made public the results obtained. The pur-

1 Weisbord, N. E.: Venezuelan Devonian fossils, Bull. Amer. Paleont.,
vol. XI, No. 46, 1926.

9

2 Liddle, R. A.: The geology of Venezuela and Trinidad, 1928, pp. 97-
101, Forth Worth, Texas.

275 Rio Cacutr1 Section: LippDLE 9

poses of the expedition up Rio Cachiri by Liddle in 1942 were:

1. To traverse westward far enough to pass through the
section and discover the nature of the rocks forming the
core and the highest peaks of the Sierra de Perija.

2. To learn if sediments older than Devonian are pres-
ent in the mountains.

3. To collect systematically from the entire pre-Cretaceous
section.

4. To determine positively the age of the “Old Red series”,
(thought to be Permian) and its relation to the Devonian
below and to the Cretaceous above.

5. To ascertain the relation of the black and red crinoidal
limestone exposed near the mouth of Cano del Norte to
the red-bed section that extends from the limestone out-
crop farther northwest up the Cano; and to find out the
relation of the crinoidal limestone to the Rio Negro
formation of Lower Cretaceous age which is at the sur-
face just east of the limestone.

6. To establish with certainty the age of the crinoidal lime-
stone, believed to be Permo-Carboniferous.

The results of this expedition are contained in the following
pages.

No attempt has been made to discuss in detail the Cretaceous
and lower Eocene sediments which outcrop in the area exam-
ined. Their presence is briefly recorded merely to indicate their
proper position in the geologic section.

ACKNOWLEDGMENTS

The success of this expedition into the Sierra de Perija was
due in a great measure to the assistance provided by Mr. R. W.
Mcllvain, Vice-President and Mr. Theron Wasson, Chief Geolo-
gist of The Pure Oil Company. Upon their instructions all ar-
rangements for my entering Venezuela were made by Dr. J. M.
Travieso Patl of Caracas, Venezuela. To obtain the necessary
permits in time of war was no small task. Mr. Wasson also fur-

8 BULLETIN 108 276

nished me with the traverse of Rio Cachiri made by Netick,
Weaver, and Madera in 1926. This survey enabled me to re-
éxamine the lower course of the river more rapidly than would
have been possible otherwise, thus permitting me to spend more
time in its upper branches.

Dr. W. H. Hegwein, Chief Geologist of the Caribbean Petrol-
eum Company, Maracaibo, Venezuela, furnished me with a map
covering much of the upper portion of Rio Cachiri. This map,
made by Dr. J. Krebs, enabled me to study and collect rapidly
from the Devonian section, thus leaving time enough to pene-
trate to the core of the Sierra de Perija.

I am especially indebted to Mr. H. L. Patterson, General Man-
ager, and to Mr. Joe Netick, Chief Geologist, of the Orinoco Oil
Company, Maracaibo, Venezuela. Without their help I could
not have completed my work during the short, dry season of the
Sierra de Perija. Mr. Netick also gave liberally from his knowl-
edge of Venezuelan geology, acquired during the past 20 years,
and made available to me all his collections. Some fossils from
these collections are figured in this work.

My wife, Pearle Goolsby Liddle, has assisted in preparing the
manuscript and Dr. Kk. V. Palmer has supervised its progress
through the press. To both I am deeply grateful.

STRATIGRAPHY
IGNEOUS ROCKS

Two complementary types of igneous rocks have been found
on Rio Cachiri east of the main core of the Sierra de Perija.
Their areal extent, however, is small because they occur only as
intrusives into sedimentary beds—the acidic and basic types on
Cano del Norte, and the basic type on Canto Grande. Acidic
igneous rocks only, in association with metamorphics, have been
discovered in the core of the mountains.

ACIDIC GROUP

One hundred meters above the junction of the Cafio del Norte
branch of Rio Cachiri with the Cafio del Oeste branch is a fairly
large pluglike mass which is well exposed in the east bank of the

Aan to CAcHIRI Srecrion: LImDpLE 9

river. It is composed of quartz syenite, or aplite, and quartz
diorite which are extremely hard to fracture, and are highly re-
sistant to erosion. It protrudes from the heavily forested moun-
tain slope into outcropping limestones that lie at the top of the
red-bed section of probable Permian age and immediately below
the Rio Negro formation,—a conglomeratic sandstone of Lower
Cretaceous (Barremien) age. Slight alteration of the limestone
beds adjacent to this igneous mass, notable mineralization and red
staining by iron, indicate clearly the intrusive nature of the mass.
Some of the limestone beds into which the intrusion was forced
are full of large crinoid stems. In one bed, in association with
a multitude of crinoid stems, is the hinge area of a Spirifer, and
a large bryozoan form. Other beds of limestone that are quite
similar in character to the crinoidal limestone contain no fossils
although both types are in contact with each other. The quartz
syenite and the quartz diorite are closely related in the mass,—
the only difference being that in the quartz syenite the grayish
ground-mass of dense, amorphous silica has crystals of glassy
quartz embedded in it, whereas, the quartz diorite contains, in
addition, specks of hornblende and traces of iron. In both types
the grayish ground-mass is splotched with pale pink and light
green.

Samples: A’ and 17.

Reddish and greenish quartz syenite and quartz diorite intrude
red shales of probable Permian age higher up on the Cano del
Norte branch of Rio Cachiri than the locality of Sample “A”.
They resemble somewhat the rock in Sample “A” but have larger
quartz crystals and angular fragments of greenstone. Some places
in the intrusion, represented by Sample OI-J-65, look like igneous
breccia.

In the core of the Sierra de Perija, in association with meta-
morphic rocks, chiefly quartzite and schist, are moderately soft,
creamy-gray, mica-hornblende granite, and veins and dikes of
vitreous, white, igneous quartz that cut both the metamorphic
rocks and the granite.

Samples: parts of 78 and 79.

10 BULLETIN 108 278

BASIC GROUP

On the Cano del Norte branch of Rio Cachiri dense, greenish-
black diorite forms the contact zone between red beds of the
Permo-Carboniferous and underlying dark-gray limestones and
shales of the Devonian. The limestones are shattered and cut
by calcite veins; the Permo-Carboniferous shales above the
diorite are deep red and impregnated with iron.

Samples: 3, 4, 5, 6, and OI-J-69.

On the Cano Grande branch of Rio Cachiri a sill of basalt has
penetrated the bedding of dark-gray shales of the Cano del Oeste
formation of Upper Devonian age baking them to glossy black
and indurating them considerably. Some mineralization by iron
has taken place. The sill is a typical, dense, very hard, black
diorite. The time at which it intruded the Devonian beds is not
known, but since on Rio Gé not far away in the same mountain
range similar basic rock has intruded Lower Cretaceous beds,
it 1s probable that the sill on Rio Cachiri is no older than Creta-
ceous ; possibly it is much younger.

Sample 61 is from this sill,

METAMORPHIC ROCKS
The only true metamorphic rocks in Rio Cachiri occur in its
headwaters where they constitute the core of the Sierra de Perija.
Mica-hornblende schist and quartzite are the only types found.
They occur in association with quartz-feldspar granite, both the

granite and the metamorphic rocks being intruded by dikes and
veins of vitreous quartz.

PRE-DEVONIAN: PROBABLY ARCHEOZOIC

Sierra de Perija Series

Name.—Sierra de Perija series is here used to designate gray-
ish-tan, very hard quartzites cut by dikes and veins of white
igneous quartz, together with mica schists and gneissoid schists
intruded by granite found in place in the headwaters of the Cano
Grande branch of Rio Cachiri, districts of Mara and Maracaibo,
State of Zulia, and evinced by abundant float in the Cano del
Oeste branch of: Rio Cachiri, and in Rio Tinacoa. In Rio Gé
quartzite boulders were found in float but no schist was seen.

x

279 Rio CACHIRI SECTION: LIDDLE ila

Stratigraphic position —The Sierra de Perija series lies below
and in faulted contact with beds of Devonian age on the Cano
Grande branch of Rio Cachiri. There is no doubt of the relation
as the contact can be located within a few feet. This series which
doubtless embraces rocks of several ages, origins, and sources
comprises the high mountain peaks of the Sierra de Perija.

Physical character.—Grayish-tan, mauve, massively bedded,
hard quartzite cut by veins and dikes of white quartz; greenish-
gray, micaceous schists intruded by cream-colored granite; and
greenish-yellow, gneissoid schists comprise the Sierra de Perija
series. Some of the quartz dikes are two and one-half feet in
width and were traced across rock faces for 20 feet. The quartz-
ite and the schistose rocks are interbedded.

Extent and thickness—From rocks in situ, and from float, it
is evident that the Sierra de Perija series comprises the core of
Sierra de Perija and forms the high peaks, at least between Rio
Apon on the south and Rio Cachiri on the north. Only 1,000
feet of the series were penetrated in the Cano Grande branch of
Rio Cachiri because of lack of time, but it can be stated confi-
dently that there are several thousand feet of this heterogeneous
series.

Age and correlation.—The Sierra de Perija series is definitely
pre-Devonian, but a more exact age cannot be ascribed. Probably
it includes rocks of several ages as 1s suggested by the character
of the rocks themselves. It is believed to be pre-Paleozoic,—
probably Archeozoic since unmetamorphosed Middle Ordovician
has been found in the Venezuelan Andes, and Lower Ordovician
and Upper Cambrian sediments are present in the Cordillera
Oriental of Colombia about 300 kilometers south of Rio Cachiri.
In both regions, which are in the Andean system, they are under-
lain by metamorphic and igneous rocks similar in character to
those forming the core of the Sierra de Perija on Rio Cachiri. -

Topographic expression and local details —Only in the head-
waters of the Cano Grande branch of Rio Cachiri have rocks of
the Sierra de Perija series been found in place, but float has been

12 BULLETIN 108 280

picked up in several of the other larger rivers which drain east-
ward from this mountain range,—notably Rio Socuy, Rio Guas-
are, and Rio Palmar. Rocks of this series form the high peaks
of the central area of this mountain chain.
Samples 78 and 79 were collected from the Sierra de Perija
series.
SEDIMENTARY ROCKS

From the core of the Sierra de Perija eastward to its foothills
where Rio Cachiri debouches from the mountains there are ex-
posed along the river Devonian, Permo-Carboniferous, Creta-
ceous, and lower Eocene sediments. The Devonian is represent-
ed by the Rio Cachiri series which has been divided from base
to top into the Cano Grande formation of fossiliferous, dark-
gray, micaceous shales of Lower and Middle Devonian age; the
Cano del Oeste formation of grayish-black, micaceous shales in-
tercalated with some grayish-brown, micaceous, quartzitic sand-
stones of probable Upper Devonian age; and the Campo Chico
formation of micaceous, quartzitic sandstones, gray, calcareous,
micaceous shales, and a few dark-gray, calcitic limestones of
probable Upper Devonian age. No fossils, either megascopic or
microscopic, have been found in the beds that are thought to be
Upper Devonian.

The Permo-Carboniferous, separated from the Devonian by a
conglomerate made up of red shale in which angular fragments
of limestone are embedded, consists of red, micaceous shales; at
the top of these are dark-gray to black, locally red-stained lime-
stones, some beds of which are full of large crinoid stems. In one
bed a Spirifer and a large, tubular Bryozoa are associated with
the crinoid stems,

all the stems being calcitized.

The Cretaceous, lying unconformably on the Permo-Carbonif-
erous, is represented by a basal conglomeratic sandstone,—the
Rio Negro formation of Barremien age, conformably overlain by
massive, grayish-white limestones and minor gray shales of the
Cogollo formation of Aptien and Albien ages. Conformably on
the Cogollo formation is La Luna formation of black, petrolifer-

2811 Rio Cacuirt Section: Lipper 15

ous limestone and shale carrying discoidal and ellipsoidal masses
of fossiliferous, petroliferous limestone. La Luna formation is
Vraconnien in age and grades imperceptibly upward into the
Guayuta shale of the Guayuta group. This shale is grayish black
and of Cenomanien and, Turonien ages. To date the only evi-
dence of Cretaceous that is younger than Turonien in the region
north of Rio Negro is the reference by Gerhardt* to Lower Sen-
onien at Hato Nuevo, in the Sierra de Perija, District of Mara-
caibo, Venezuela. This locality, however, is not in Venezuela
but is a short distance to the west in the Department of Magda-
lena, Colombia. At Rio Negro, though, Maestrichtien Cretaceous
is represented by coarse, gray sandstone in Quebrada del Mene,
a branch of the river. This quebrada parallels on the west the
frontal ridge of the mountains which, at this place, is made up
of La Sierra sandstone, the guebrada extending along the contact
between the sandstone on the east and Upper Cretaceous shales
on the west. Faulting has narrowed the shale valley so that it
is not known how much of the Guayuta or Colon is missing.
Fossils indicating this occurrence of Maestrichtien are Cucullea
pertjana F. and H. Hodson, and Pseudocucullea perijana Harris,
F. and H. Hodson‘.

The Eocene, which seems to rest with structural, as well as
stratigraphic unconformity, on the Upper Cretaceous, has at its
base the Rio Guasare formation. It is a marly, calcitic, red-
splotched, fossiliferous, impure limestone (in places an oyster
reef) that grades upward into coal-bearing shales and sandstones
of the Third Coal horizon or Paso Diablo formation which com-
prises the basal portion of the Misoa-Trujillo formation of lower
Eocene age. Resistant sandstones and lignitic shales of the Third
Coal horizon form the frontal barrier or ridge of the mountains
on Rio Cachiri at Playa La India but the formation extends much
farther eastward into the great syncline which lies between the:
foothills of the Sierra de Perija on the west and Cerros Los

8 Gerhardt, K.: Beitrdge zur Kenntniss der Kreideformation in Vene-

zuela und Peru, Neues Jahr. Min., Beil. Bd. XI, 1897-98, pp. 69-70.
nt Hodson, F. Hodson, H. K. and Harris, G. D.: Some Venezuelan and
Caribbean mollusks, Bull. Amer. Paleont., vol. XVIII, No. 49, 1927, pp- 1-2.

14 BULLETIN 108 282

Guineos on the east. It also outcrops to the southwest in Ar-
royo Cerrejon in the Valley of Rio Rancheria, Department of
Magdalena, Colombia.

PALEOZOIC
Lower and Middle Devonian: Rio Cachiri Series
Cano Grande Formation

Name.—In 1928 Liddle® referred to his Rio Cachiri series all
sediments below the red beds on the Cano del Norte branch of
Rio Cachiri as far as the locality of his deepest penetration into
the Devonian section. His expedition of 1942, in which a de-
tailed study of the Devonian was made, and a systematic collec-
tion of samples secured, clearly indicates that although all sedi-
ments here referred to the Devonian have a distinct lithological
relationship they can be divided into three formations,—the old-
est of which is highly fossiliferous in places.

Stratigraphic position.—In the headwaters of the Cano Grande
branch of Rio Cachiri the fossiliferous Cano Grande formation
is in fault contact with the core of the Sierra de Perija. Ex-
tremely hard, slaty shale and quartzitic sandstone (Samples 77
and 7714) which contain imprints of Lower Devonian fossils
comprise the oldest Devonian beds found, They rest with dis-
tinct unconformity on schists, quartzites, granite, and quartz of
the Sierra de Perija series that may be Archeozoic in age. The
Cano Grande formation grades upward into the Cano del Oeste
formation which constitutes the middle portion of the Rio Cachiri
series,—the contact being placed between the localities of Samples
62 and 63. At this stratigraphic level there is a notable though
gradual lithologic change, and an abrupt termination of an
abundant and varied fauna.

Physical character.—TVhe Cano Grande formation is a distinct
lithologic and biologic unit. Gray, micaceous, nodular, limoni-
tic, calcareous, sandy shales containing mud pellets, microscopic
particles of lignitic matter, and breaking with a shattery fracture,
carry a prolific Lower and Middle Devonian fauna. In the ex-

5 Liddle, R. A.: op. cit., pp. 97-99.

283 Rro Cacniri Section: LIDDLE 15

treme basal portion are some evenly bedded, fine-grained, dark-
gray, micaceous, quartzitic sandstones, and a few more shaly
sandstones which contain imprints of Spirifers and corals.

Extent and thickness—The Cano Grande formation of the
Rio Cachiri series has been found in place in the Sierra de
Perija only in the headwaters of Rio Cachiri. It is present in all
branches of the river. Float from this formation has been collect-
ed at the mountain front in Rio Socuy and in Rio Guasare which,
like Rio Cachiri, flow eastward down from the northern end of
the Sierra de Perija.

The thickness of the Cano Grande formation is calculated to
be at least 2,500 feet. Accurate measurement is impossible be-
cause of faulting and intervals that are concealed by dense forests.

Age and correlation.—The prolific, well-preserved fauna of the
Cano Grande formation is positive proof of its Lower and Mid-
dle Devonian age,—ranging from Helderbergian through Orisk-
anian and Hamiltonian. It can be correlated with the Floresta
fauna of Colombia described by Caster® even though there are
some differences that may be accounted for by facies changes,
since the localities are 300 kilometers apart in the same mountain
system. The Floresta fauna seems to more nearly represent the
Helderbergian and Oriskanian, and to have less of a Hamilton-
_lan character, whereas, in the Cano Grande fauna the Hamilton-
ian is well represented. There is a close lithologic and faunal
relation between the Rio Cachiri series and Lower and Middle
Devonian sediments of New York State. However, as would be
expected in areas so far apart, some of the fauna is quite differ-
ent. Lithologically the Rio Cachiri series bears little resemblance
to the Floresta beds.

Fossils identified by Harris and Wells from the Cafo Grande

formation are:

Heliophyllum halli Mime Edwards and Haime
Heterophrentis venezuelensis (Weisbord)
Synaptophyllum vermetum (Weisbord)
Zonophyllum, sp.

Crinoid stems

6 Caster, K. E.: A Devonian fauna from Colombia, Bull. Amer. Paleont.
vol. XXIV, No. 83, 1939, pp. 1-218.

16 BuLLETIN 10S 28+

Menestella venezuelensis Weisbord
Polypora cachirita Weisbord
Aetimopteria subulrichi, n. sp.
?Aviculopecten yeakeli Weisbord
Aviculopecten, sp. (fragment)
Ctenodonta?, sp.

Jdmondia sylvana Hartt

Limoptera tenuis, n. sp.

Nucula?, sp.

Sehizodus venezuclanus, n. sp.
Platyeeras gibralteri, n. sp.

Platyceras sinistrum, h. sp.
Platyostoma ventricosum (Conrad)
Piatyostoma ventricosum var. permudum, n. var.
Acrospirifer olssoni Caster

Amphigenia elongata var. weisbordi, n. var.
Athyris spiriferoides (Eaton)

Atrypa reticularis var. harrisi Caster
Camarotechia, sp.

Chonetes stiibeli Ulrich

Chonetes venezuelensis Weisbord
Dalmanella ef. nettoana Rath
Dictrosirophia cooperi Caster

lulytua colombiana Caster

Klytha? plana, n. sp.

Hodevonaria imperalis Caster
Wodevoneria subi emispherica Weisbord
Leptena rhomboidalis, (Wilkens) vars.
Leptrostrophia caribbeana Weisbord
Leptrostrophia concinna (Morris and Sharpe)
Meristella, sp. :

Meristella wheeleri Caster

Pentagonia? gemmisulcata Caster
Produetella, sp.

Rhipidomella liddlei, n. sp.
Schellwienella goldringe Caster
Spirifer kingi Caster

Spirifer olssoni Caster

Spirifer, sp. (fragments)

Spirifer weisbordi, n. sp.
Stropheodonta (Cymostrophia) casteri, n. sp.
Stropheodonta kozlowskii Caster
Strophonella? meridionalis (Caster)
Tropidoleptus carimatus Conrad

Shark tooth

Topographic expression and local details—Actual outcrops of
the Cano Grande formation in the several branches of Rio

Cachiri, and brief glimpses of the mountains which it sustains,

285 Rio Cacuiri Srction: LIppLE ay

that can be seen occasionally from the river, comprise our general
knowledge of the topographic influence of this formation. In
the river the harder calcareous shales form vertical cliffs in
places over 100 feet high, as well as narrow, vertical- and over-
hanging-walled canyons, and low waterfalls. Narrow, sharp
valleys have been cut into the softer shales. A surprising fea-
ture is the hardness of the shale in cliff faces, considering the
readiness with which it shatters after exposure, and the rapidity
with which it weathers when soaked in water.

Samples: OI-J-97 (float), Ol-J-113 (float), 31 (float), 34
(float), 37, 38 (float), 39, 40, 41, 42, 43, from the Cano del Oeste
branch of Rio Cachiri, and

Samples,:\635(645/05: 66, (67, (68; 60) 70,7, 72, Fenian Zoe 70;
77, 77Yo, from the Cano Grande branch of Rio Cachiri.

The Cano Grande formation was not reached on Cano del
Norte by the 1942 expedition of Liddle. It was examined in
1924 by the expedition of Yeakel, McFarland, and Liddle and
some of the fossils collected by them were described by Weisbord’.

Upper Devonian
Catto del Oeste Formation

Name.—The Cano del Oeste formation is named from the Cano
del Oeste branch of Rio Cachiri where it is well exposed between
traverse stations 32 and 42. It was thought, at first, that sedi-
ments comprising this formation could be referred directly to
the Rio Tinacoa formation which is an established name but since
no fossils have been found in either formation it is more advisable
to introduce a local name and suggest a correlation between the
two formations.

Stratigraphic position The Cano del Oeste formation, where
the Devonian is in normal sequence, separates the Cano Grande
formation from the Campo Chico formation, There seems to be,
a perfect gradation from base to top of the entire Devonian sec-
tion. However, there is enough difference between the three

« Weisbord, N. E.: op. cit., pp. 1-52.

18 BuLLETIN 108 286

parts to warrant separate formational names.

Physical character.—On Rio Cachiri the Cafio del Oeste for-
mation is composed of bluish-black, fine-grained, micaceous, fer-
ruginous quartzite ; dark-gray, micaceous, nodular, limonitic, un-
fossiliferous shale which has a shattery fracture and contains mi-
croscopic particles of lignite ; black, micaceous, slaty shale having
a splintery nature, and some black, unctuous, twisted unfossilifer-
ous shale. Local induration of the shale in the basal part of the
formation is caused by a 30-foot sill of basalt. On either side of it
the shales are slaty.

In the type section of the Rio Tinacoa formation on Rio Tina-
coa the shale which comprises most of the formation is squeezed,
twisted, and crumpled more than the shale of the Cano del Oeste
formation on Rio Cachiri, or shale of the same horizon on Rio
Macoita. On Rio Tinacoa the Rio Tinacoa formation is predom-
inantly black, nodular shale which breaks conchoidally or splint-
ery. There is much slickensiding, and in some places the black
shale appears to be graphitic. In the lower one-third of the sec-
tion are some thinly bedded, hard, quartzitic sandstones, and in
the basal part some thinly bedded, black, hard limestones.

Extent and thickness.—The Cano del Oeste formation and the
Rio Tinacoa formation are known to reach, in the Sierra de
Perija, at least from Rio Macoita on the south to Rio Cachiri on
the north, although they are not exposed locally in the interven-
ing area on rivers like La Luna which do not penetrate deep
enough into the section. ‘They are present, only in part, on some
other rivers because of faulting. On account of the terrific
crumpling and twisting which accompanies the faulting in the Rio
Tinacoa formation on Rio Tinacoa, an accurate estimate can not
be made of its thickness, but on Rio Cachiri where the section is
less disturbed there are about 3,500 feet of the Cano del Oeste
formation.

lge and correlation.—No fossils have been found yet in the
Cano del Oeste formation, but it is known to lie with gradational

287 Rro Cacutr~ Srerion: Lippip 19

conformity above the Cano Grande formation of Lower and
Middle Devonian age and consequently is thought to be Upper
Devonian. It is believed to correlate with the Rio Tinacoa for-
mation which has been described by geologists of the Caribbean
Petroleum Company from the section on Rio Tinacoa already
mentioned.

Topographic expression and local details.- -Thinly bedded,
quartzitic sandstones and a few, thin limestones of the Cafio del
Oeste formation protect the intercalated, softer shales but where
they are not present and the shales stand at steep angles, landslides
are common. In general, the formation supports high, rugged
mountains.

Samples: 57, 58, 59, 60, 62, on the Cafio Grande branch of Rio
Cachiri, and

Samples 32, 33,34, 35, 30, 37, 38, 39, 40, 41, on the Cafio
del Oeste branch of Rio Cachiri.

Campo Chico Formation

Name.—The Campo Chico formation is named from the lo-
cality of an overnight camp on the Cafio Grande branch of Rio
Cachiri. There is no particular topographic or drainage feature
within the area of outcrop of these sediments so the camp site
was utilized as a name although it may not meet the exact re-
quirements of nomenclature.

Geologists of the Caribbean Petroleum Company use the term
Rio Macoita formation to designate thinly bedded, sandy, mica-
ceous, gray shales and dark-gray, evenly bedded, quartzitic, fine-
grained sandstones which are well exposed on Rio Macoita, in
thet sierra de’Perija, State of Zulia. To date no fossils have been
found in these beds, but on lithology they are correlated with the
Campo Chico formation. Hedberg and Sass* have used :the term
“Macoita series” to replace the term “Old Red series” of the
Sierra de Perija area, but unfortunately the type section which
they designate for their “Macoita series” on Rio Macoita con-

8 Hedberg, H. D., and Sass, L. C.:Sinopsis de las formaciones geolo-
gicas de la parte occidental de la Cuenca de Maracaibo, Venezuela, Bol.
Geol. y Min., t. 1, Nos. 2, 3, y 4, 1937, p. 79.

20 BULLETIN 108 288

tains no beds previously known as the “Old Red series”. On
Rio Macoita there is an unconformity which places the io
Negro formation directly in contact with the Rio Macoita forma-
tion, the red-bed section apparently being cut out by the uncon-
formity. For this reason Hedberg and Sass’ usage 1s dropped
and that in use by geologists of the Caribbean Petroleum Com-
pany is adopted.

Stratigraphic position—On Rio Cachiri the Campo Chico
formation lies below Permo-Carboniferous, probably Permian,
red beds from which it is separated by a conglomerate composed
of deep-red, micaceous shale in which are embedded angular
fragments of bluish-gray limestone. Although it is not possible
to determine with certainty, it is believed that an unconformity
of magnitude separates the Campo Chico formation from the
overlying red beds. This is confirmed by the absence of the
Mississippian and probably much ot the Pennsylvanian. There
is complete conformity between the Campo Chico formation and
the Cano del Oeste formation which directly underlies it.

Physical character.—Dark-gray, hard, evenly bedded, quartz-
itic sandstones intercalated with dark-gray, hard, micaceous
shales comprise most of the Campo Chico formation. There are
also, a few thin, hard, black, calcitic limestones.

Extent and thickness—Because of intense disturbances in the
type section of the Rio Macoita formation on Rio Macoita, and
in its outcrop on Rio Tinacoa, its thickness cannot be determ-
ined accurately. On Rio Cachiri, where less disturbance has
taken place, there are, at least, 2,000 feet of the Campo Chico
formation. On other rivers, between Rio Tinacoa on the south
and Rio Cachiri on the north, only parts of the Rio Macoita form-
ation or the Campo Chico formation are present, This is par-
ticularly true of Rio Gé, where a diorite intrusion is in contact
with the Rio Macoita or the Campo Chico formation on the east ;
in fact, it occupies all the area between this horizon and the Cog-
ollo formation of the Lower Cretaceous. Similar igneous rocks
separate the Rio Macoita or Campo Chico formation from sedi-
ments exposed farther west.

289 Rro Cacutri SEctTIoN: LIDDLE 91

On most rivers in the northern part of the Sierra de Perija,
which cut deeply enough into the mountains to reach the Campo
Chico or Rio Macoita formation, there is some portion of this
formation exposed. Of the rivers in this region which have been
examined, the best exposures were found on Rio Cachiri and
Rio Macoita.

Age and correlation.—The Campo Chico formation is thought
to belong in the Upper Devonian because on Rio Cachiri there
is no visible structural or lithologic break between it and the Cano
del Oeste formation below, or between the Cano del Oeste for-
mation and the underlying Cano Grande formation,—the Lower
and Middle Devonian age of which is definitely established by
fossil remains. However, there is sufficient lithologic change
to substantiate the three parts into which the Devonian is sep-
arated. From base to top these are: Cano Grande formation,
Cano del Oeste formation, and the Campo Chico formation. The
Campo Chico formation is correlated with the Rio Macoita for-
mation on lithology only as no fossils have been found in either
formation.

Topographic expression and local details—The resistance of
the Campo Chico or Rio Macoita formation to erosion enables it
to support many vertical bluffs along rivers where it outcrops.
Mountains at a distance from the rivers have the same charac-
teristic bluffs and steep slopes.

Samples: 53, 54, 55, 56, on the Cano Grande branch of Rio
Cachiri;

“Samples: 20, 21, 22, 24, 25, 26, 27, on the Cafio del Oeste
branch of Rio Cachiri, and

Samples: 1, 2, “C,” on the Cafio del Norte branch of Rio
Cachiri.

DEVONIAN—-PERMO-CARBONIFEROUS RELATIONSHIP

No actual discordance of dip on Rio Cachiri was observed be-
tween the Devonian and the overlying red beds which are consid-
ered to be Permo-Carboniferous,—probably Permian in age.

22 BULLETIN 108 290)

However, in sediments standing at such high angles, where out-
crops are separated by dense forests, divergence in dip, unless of
magnitude, is difficult to detect. Unconformity is evinced, how-
ever, by the absence of some of the Carboniferous beds which
are present in the Colombian and Venezuelan Andes, and by a
25-foot conglomerate at the base of the red-bed section at its con-
tact with the Devonian below. This conglomerate has a matrix
of red, micaceous shale in which are embedded angular frag-
ments of light- and dark-gray limestone. The source from which
this limestone was derived is not clear. Very little limestone was
found in the Devonian, and it 1s surprising that sandstone frag-
ments were not found in the conglomerate, since quartzitic sand-
stone is common in the Campo Chico formation just below the
red beds. The limestone fragments may come from a horizon
not present on Rio Cachiri, being cut out by the unconformity
between the Devonian and the Permo-Carboniferous. Further-
more, as is indicated by fossiliferous float from Station OI-J-113,
there appear to be Carboniferous beds within the drainage of Rio
Cachiri which to date have not been found in place in the river
itself. Fossils from the float are Leptodomus ulrichi Clark .and
Productus liddlei, n. sp.

Permo-Carboniferous

Palmarito Series

Name.—The Palmarito series was introduced by Christ® to
include rocks of Permo-Carboniferous age in the Venezuelan
Andes. Although only a part of the Permo-Carboniferous, prob-
ably just the Upper Permian, is present on Rio Cachiri it is as-
signed to the Palmarito series in order to avoid introducing a
new name. Should it be learned later that a new name is desir-
able it can be introduced.

Stratigraphic position —A basal conglomerate which lies at
the bottom of the red-bed section constitutes the oldest rocks of

9 Christ, P.: La coupe geologique le long dw chemin de Mucuchachi a
Santa Barbara dans les Andes V énézuéliennes, Kelog. Geol. Helv., vol. XX,
No. 3, 1927.

291 Rio CacHiri SEctTION: LIDDLE oD

the Palmarito series on Rio Cachiri. It is well exposed at the
localities of Samples 52 and 53-A on the Cano Grande branch of
the river. On the Cano del Norte branch an intrusion of dior-
ite separates the Palmarito formation from the Campo Chico
formation. On the Cafio del Oeste branch faulting and concealed
section have obscured the contact of the Permo-Carboniferous
and the Devonian. Even on the Cano Grande branch the actual
contact of the two series was not seen, although the heavy forest
which blankets the contact hides but a few feet of section. There
does not appear to be much discordance in dip between the De-
vonian and the Permo-Carboniferous on Cano Grande although
a small variation would be difficult to detect in beds which are
so steeply inclined.

The contact of the crinoidal limestones, which constitute the
upper member of the Palmarito series, and the Rio Negro for-
mation of Lower Cretaceous (Barremien) age is likewise not
exposed, although the two series are only a few feet apart. It is
evident though, that the Cretaceous beds are much less inclined
than are those of the Permo-Carboniferous. However, a mass
of syenite and diorite which has intruded the crinoidal limestone
horizon at the top of the Palmarito series probably is responsible
for some of the disturbance in these Permo-Carboniferous lime-
stones. But considering the divergence of dip between the two
series, together with the fact that no Triassic or Jurassic is pres-
ent although both are exposed not far distant in Venezuela and
in Colombia, indicates an unconformity of great magnitude be-
tween the Permo-Carboniferous and the Cretaceous.

Physical character—Deep-red, micaceous shale in which are
embedded angular fragments of light- to dark-gray limestone
comprises the basal conglomerate of the Palmarito series. Above
it are deep-red, micaceous, well-bedded, unfossiliferous, brittle,
sandy shales which in some places appear to have microscopic
particles of lignitic matter; deep-red, unfossiliferous, unctuous,
compact shales having greenish-white splotches and breaking
with a shattery fracture; grayish-black, locally red-stained, cal-
citic limestone containing a profusion of large crinoid stems and
roots, a Spirifer, and a large, branching, tubular Bryozoa. The

24 3ULLETIN 108 292

crystalline tex‘ure of the limestone, its calcitization, and red
staining may be due to it being intruded by a mass of quartz
syenite and quartz diorite.

Extent and thickness——The red-bed part of the Palmarito se-
ries outcrops on all branches of Rio Cachiri. Similar red beds
have been examined on Rio Tinacoa where they are well ex-
posed; at their top and in fault contact with them are black and
red, highly shattered, silty, unfossiliferous shales which are lo-
cally slickensided. Where shattered, the shales carry abundant
calcite veins. On Rio Tinacoa no fossils were found in any of
the red-bed section and no trace of the limestones that occur at
the top of the red-bed section on Rio Cachiri were discovered.
On Rio Macoita the red beds and the limestones are missing in
the unconformity between the Rio Negro formation of Lower
Cretaceous age and the Rio Macoita formation of Upper De-
vonian age. On Rio Tinacoa there is ~ great fault between red
beds of the Palmarito series and black sales of the Rio Tinacoa
formation. It appears to have cu out most or all of the Rio
Macoita formation.

The red beds of the Palmarito series are present throughout
much of the northern part of the Sierra de Perija, but limestones
at the top of the series have been found only in one locality on
Rio Cachiri. On Rio Cachiri there are at least 1,500 feet of red
shales and from 50 to 75 feet of limestone at their top, all of
which are considered to be Permo-Carboniferous.

According to Hedberg and Sass!°:

Rocks containing Fusulina of Carboniferous age have been reported from
the upper course of Rio Palmar, Distriet of Maracaibo.

These sediments also mav ‘-elong in the Palmarito series and
be related to the Permian roci.- outcropping on Rio Cachiri.

Age and correlation.—Black an’ red crinoidal limestone beds
and the associated, similar but unfossiliferous limestones which
le at the top of the red-bed section on the Cafio del Norte branch
of Rio Cachiri resemble the top of the Palmarito series that is
exposed in the Venezuelan Andes.

The age of the Palmarito series on Rio Cachiri is not positive

10 Hedberg, H. D. and Sass, L. C.: op. cit., p: 79.

293 Rro Cacutrt Section: LippLE 25

but the evidence (Samples “F’’, 15, and 16) is believed to war-
rant its assignment to the Permo-Carboniferous,—probably the
Permian. The red and black limestone contains a large, branch-
ing form resembling Rhombopora or Alveolites, and the hinge
area of a fairly large species of Spirifer. Thin-sections of some
pieces of the limestone reveal a few Textulariatike Foramin-
ifera.

Topographic expression and local details —The black and red
crinoidal limestones which lie at the top of the red-bed section
and immediately below the Rio Negro formation in the Cano
del Norte branch of Rio Cachiri were not found in place or in
float in the Cano del Oeste branch which is very close by, or in
the Cafo Grande branch which is farther removed from Cano del
Norte, although the localities at which they normally should out-
crop were searched with care. They may be absent on these
branches of Rio Cachiri because of a variable unconformity be-
tween the Cretaceous and the Permo-Carboniferous. The red-
bed section is present on all branches of Rio Cachiri, although
faulting has complicated it with the Campo Chico formation of
Upper Devonian age on Cano del Oeste.

Kundig' makes the following reference to Permo-Carbonifer-
ous rocks on Rio Cachiri:

Upper Carboniferous developed as a sandy shale-sandstone group con-
taining typical Upper Carboniferous and possibly Lower Permian fossils
(Fenestella, Naticopsis, Orthotetes, Crenistria) was described in a previous
report a long time ago by J. Krebs from the Sierra de Perija (Rio Cachiri).

A copy of Krebs’s map was kindly furnished Liddle by Dr.
Hegwein, Chief Geologist of the Caribbean Petroleum Company,
Maracaibo, Venezuela, in order that Krebs’s locality for the fos-
sils mentioned might be found. His locality (Samples 63, 64,
and 65) was identified but the fauna is not Permo-Carbonifer-
ous but is Lower and Middle Devonian.

Samples Di 7.10, TOs 1e) ia 15, 16, on the

11 Kindig; E.: Las rocas Pre-Cretaceas de los
Venezuela con algunas observaciones sobre su

Min., t. II, Nos. 2, 3, y 4, 1939, p. 30.

Andes Centrales de
tectonica, Bol. Geol. y

26 BuLuETIN 108 294

Cano del Norte branch of Rio Cachiri,

Samples: 18, 23, 28, 29, on the Cafio del Oeste branch of the
river where the Permo-Carboniferous is complicated by having
beds of the Campo Chico formation faulted into it, and

Samples: 51, 52, and 53-A, on the Cafio Grande branch of the
river.

PERMO-CARBONIFEROUS—CRETACEOUS RELATIONSHIP

There is a distinct structural disconformity between the crin-
oidal limestones which mark the top of the Permo-Carboniferous
on the Cano del Norte branch of Rio Cachiri and the oldest
(Barremien) Cretaceous which is represented by the Rio Negro
formation. How much of this discordance of dip is due to local
intrusion of quartz syenite and quartz diorite into the limestones
is not known, for at no other place was this limestone horizon
found,—the red-bed section being separated from the Lower
Cretaceous by detrital from the surrounding mountains. How-
ever, since Barremien beds are the oldest Cretaceous on Rio
Cachiri (but in Colombia Hauterivien and Valanginien together
with Jurassic and Triassic have been found), it is reasonable to
suppose that an unconformity of great magnitude separates the

Rio Negro formation from the Palmarito formation on Rio
Cachiri.

MESOZOIC
All Mesozoic sediments in the Sierra de Perij4 on Rio Cachiri
are Cretaceous in age. They are represented from base to top
by: the Rio Negro formation of the Barremien: the Cogollo for-
mation of the Aptien and Lower Albien; the Guayuta group of
the Upper Albien, Cenomanien, and Turonien. This group in-
cludes in its basal part La Luna formation of the Albien and

Cenomanien (Vraconnien) overlain by the Guayuta shale of the
Cenomanien and ?Turonien.

The sandstones and conglomerates of the Rio Negro formation
grade upward into massive, gray limestone and_ intercalated
gray, sandy shales of the Cogollo formation.

It, in turn, is con-
formably overlain by I

-a Luna formation composed mainly of

ee a ae es Oc ae ea oe :
lack, petroliferous limestone,—the limestone grading upward in-

295 Rio CAcHIRI SECTION: LIDDLE 27

to grayish-black, locally nodular, poorly fossiliferous shales of
the Guayuta group.

In that portion of the Sierra de Perija which is north of Rio
Negro no Cretaceous younger than Turonien has been found.
It was probably deposited but has been cut out by faulting, un-
conformity, and overlap of younger beds. At Rio Negro coarse,
gray sandstone of Maestrichtien age outcrops in Quebrada del
Mene a branch of Rio Negro which joins that river just west of
the frontal barrier near La Escalera, southwest of Machiques in
the District of Perija. Cucullea perijana F. and H. Hodson and
Pseudocucullea perijana, F. and H. Hodson, in the sandstone in-
dicate its age, and there is little doubt but that it once extended
through the Sierra de Perija region.

At approximately the contact of La Luna limestone with the
Guayuta shale on Rio Gé are layers of bright-green glauconite
which carries a very meager microscopic fauna and no megascop-
ic fossils.

There is no evidence of Triassic or Jurassic on Rio Cachiri.

Lower Cretaceous
Rio Negro Formation

Name.—Hedberg and Sass’? introduced the name Rio Negro
conglomerate which they report was originated by geologists of
the Venezuelan Gulf Oil Company to designate the thick sedi-
mentary conglomerate lying conformably below the Cogollo lime-
stone on Rio Negro in the west central part of the District of
Perija, State of Zulia. This is the same formation which Liddle
called Basal Cretaceous conglomerate.

Stratigraphic position—The Rio Negro formation on Rio
Cachiri, and, in fact, throughout its exposed area in the Sierra
de Perija, lies conformably below limestones and shales of the
Cogollo formation. It rests, in all places observed, unconform- -
ably upon various older rocks. Locally in the Totumo region
it lies directly upon grano-diorite of an old land mass, whereas

12 Hedberg, H. D. and Sass, L. C.: op. cit., pp. 79-81.
13 Liddle, R. A.: op. cit., pp. 119-120.

28 BULLETIN 108 296

on Rio Cachiri, it rests unconformably upon black and red crin-
oidal limestones of Permo-Carboniferous age which are placed
in the top of the Palmarito series. On Rio Tinacoa the Rao
Negro formation of coarse, grayish-brown sandstone and inter-
calated black, calcareous shale lies above (east of) black, calcar-
eous shale which is highly shattered and impregnated with cal-
cite veins. Detrital material conceals the contact itself. A fault-
ed and crushed zone in a bluff in the southeast bank of the river
marks the contact of the black, calcareous shale and calcite-im-
pregnated limestone with red, shaly limestone below,—the red
limestone introducing a thick, red-shale section of probable Perm-
ian age.

On Rio Macoita the Rio Negro formation rests unconform-
ably upon the Rio Macoita formation in the absence of interven-
ing sediments.

Physical character—The Rio Negro formation varies locally
in character, depending upon its source. On Rio Cachiri it is
a sandstone composed of fairly well-assorted quartz and feldspar
but having less than the usual amount of conglomeratic matter.
There are no black shales in it as there are on Rio Tinacoa. It
is of moderate hardness and lacks the thin, quartzitic layers found
in some other places. By way of contrast it should be mentioned
that on Rio La Luna, the kio Negro formation 1s composed al-
most entirely of small and large igneous fragments. Some of the
large fragments are 3 to 4 inches in diameter. All of them are
embedded in red shale and very fine, silty, red sandstone. On
Rio Tinacoa the Rio Negro formation is a fairly fine, gray sand-
stone made up of angular quartz crystals and feldspar. Inter-
bedded with the sandstone is some black shale. The sandstone
contains considerable ferruginous matter.

Extent and thickness—The Rio Negro formation is known to
be present in the Sierra de Perija, at least between Rio Guasare
on the north and Rio Yasa on the south, though it probably exists
farther north, and without doubt, farther to the south.

On Rio Cachiri it occupies a narrow belt below, or west of,

the cerro-forming Cogollo limestone. It has no particular influ-

207 Rio CacnHtrr1 SECTION: LIDDLE 29

ence on topography.

As would be expected from a basal conglomerate, the Rio
Negro formation, even in the rather limited area of the Sierra de
Perija, is extremely variable in thickness. On Rio Cachiri it is
200 feet thick.

Age and correlation._-The Rio Negro formation represents
the oldest Cretaceous in the western part of Venezuela. No fos-
sils have been found in the formation itself but as it lies conform-
ably below the Cogollo formation of Aptien-Albien age, it is be-
lieved to be Barremien. It is considered to be an equivalent of,
at least, a portion of the Barranquin formation of the eastern part
of Venezuela, which in addition to conglomeratic sandstones,
carries dark-gray shales and gray limestones that contain Lower
Aptien and Barremien fossils.

Topographic expression and local details—The small amount
of the Rio Negro formation present on Rio Cachiri, and its rela-
tive resistance being about equal to that of the underlying Permo-
Carboniferous sediments, gives it no particular influence on
topography ; in fact on the Cano Grande branch of the river it is
difficult to find.

No samples were collected.

Cogollo Formation

Name.—The Cogollo formation, which is usually referred to as
the Cogollo limestone because of the predominance of grayish-
white limestone in it, is well exposed at the type locality on Rio
Cogollo 40 kilometers south of Rio Cachiri but still in the Sierra
de Perija. It was described as the Cogollo limestone by Garner™
in 1920,

Stratigraphic position—The Cogollo formation lies with per-
fect conformity above the Rio Negro formation, and below La
Luna formation of the Guayuta group. In places the contacts’
appear to be gradational; in others, though conformable, there

14 Garner, A. H.: Suggested nomenclature and correlation of geologi-
cal formations in Venezuela, Trans. Amer. Inst. Min. and Met, Engrs.,
1926, pp. 677-684.

30 BULLETIN 108 298

is a distinct lithologic change at the contact levels.

Physical character —Massively bedded, gray limestones with
which are intercalated minor, sandy, gray shales comprise the
Cogollo formation, the limestones being so dominant that they
vive the impression that the formation is composed of limestone
only. Cross-sections of fossils replaced by calcite are visible on
weathered surfaces of the thicker limestone ledges. They are
principally species of Requienia, Ostrea, Homomya, Trigonia, and
[socardia. From the sandy shale horizons casts of these fossils
and ammonites have been secured. In weathering, the massive
beds of limestone become pitted and cavernous, especially where
they tower to high, vertical bluffs, and steep canyon walls.

Extent and thickness —On Rio Cachiri the Cogollo formation
is 1,400 feet thick and very prominent. Throughout its exposed
area in the Sierra de Perija, where not thinned by faulting, it 1s
uniform in character and thickness.

Age and correlation—The Lower Cretaceous, Aptien-Albien,
age of the Cogollo formation is positively established by the fos-
sils which it contains. Its correlation with El Cantil formation
of the eastern part of Venezuela is exact.

Topographic expression and local details.—Vertical and over-
hanging, white-walled gorges choked with giant limestone boul-
ders in Rio Cachiri, and prominent white-faced mountain peaks
at distances from the river, characterizes the outcrop of the
Cogollo formation. On all rivers in the Sierra de Perija, which
cut into the formation, its expression is similar. It is especially
noticeable because of the less resistant Rio Negro formation be-
low, and the soft Guayuta group above.

No samples were collected from this formation on Rio Cachiri,
but a fair collection was made on Rio Gé.

Middle Cretaceous: Guayuta Group

La Luna Formation

Name.—-In 1926 Garner’ described La Luna limestone from
Rio La Luna which is a small stream that emerges from the

15 Garner, A. H.: loc. cit.

Rio Cacutri Section: LippLE 31

iS)
a)
co)

Sierra de Perija at a little hacienda called Rancho La Luna.

Stratigraphic position —La Luna formation lies with absolute
conformity upon the Cogollo formation. In some places there is
evidence of gradation, but in others the contact is fairly sharp,
occurring at the upper limit of the massively bedded, gray lime-
stones of the Cogollo, where they are overlain by dark-gray to
black, petroliferous limestones and carbonaceous shales of La
Luna. However, at the type locality on Rio La Luna the amount
of beds included in La Luna formation is much greater than at
other places in the Sierra de Perija. It appears that the sea was
deeper here than in other localities and as a result limestone de-
position reached much higher in the section. Consequently,
identification and correlation of similar black limestones and
shales containing black, ellipsoidal or discoidal, petroliferous
limestone masses in the Guayuta group are hazardous unless the
contained faunas are confirmative. Furthermore, limestone hor-
izons in the type section of La Luna are represented by shales in
nearby areas.

A gradational relation exists between La Luna formation and
the overlying Guayuta shale of the middle part of the Guayuta
group which is composed mainly of dark-gray to black, locally
nodular shales that carry few large fossils.

Physical character.—Black, thinly bedded, petroliferous, local-
ly shaly limestones with which are intercalated black, sandy, car-
bonaceous shales containing black, discoidal and ellipsoidal, petro-
liferous, fossiliferous limestone masses of various sizes make up
most of La Luna formation. The lenticular limestone masses
are so well developed in horizons that they form continuous lay-
ers. Some contain many fossils,—chiefly pelecypods, and am-
monites whose body cavities occasionally hold asphaltic oil, Ir-
regular masses of black chert characteristically occur in the basal
part of La Luna formation, especially on the Cafio Grande branch
of Rio Cachiri and on Rio Tinacoa.

In the type locality of La Luna formation on Rio La Luna the
dark-gray shales grade upward into light-gray, ashy shales simi-
lar to gray, ashy shales of the upper part of the Guayuta group

32 BULLETIN 108 300

in the eastern part of Venezuela. In one horizon in the type lo-
cality these grayish-white, ashy shales carry perfectly spherical
limestone balls that are not fossiliferous. The manner in which
these ellipsoidal and discoidal limestone masses, as well as the
spherical balls, were formed is but partially known. They are
embedded in the shales—the laminz of the shales curving con-
formably about them suggest their origin in pockets in the sea
floor around nuclei of fossils or foreign matter, the limestone de-
position or growth taking place while the surrounding shales
were being laid down. The lenticular masses vary from a few
inches to several feet in diameter, the spherical balls from less
than an inch to 10 inches in diameter. The upper part of La
Luna formation carries a pelagic fauna; the lower part of the
formation does not.

Extent and thickness —La Luna formation on Rio Cachiri is
600 feet thick. On most other rivers in the northern part of the
Sierra de Perija where it is exposed, with the exception of Rio
La Luna, it varies from 200 to 600 feet. In the type section on
Rio La Luna there are between 1,100 and 1,200 feet.

Age and correlation The fauna of La Luna formation indi-
cates that the lowest beds are Upper Albien in age. Excluding
the type locality, the upper range of the main limestones is
Cenomanien. At the type locality the uppermost limestones and
shales are poorly fossiliferous but the fauna indicates ?Turonien.
La Luna is principally a Middle Cretaceous (Vraconnien) hori-
zon.

In the Venezuelan Andes also, La Luna limestones form the
basal part of the Guayuta group where the group is present.

In the eastern part of Venezuela La Luna formation comprises
the basal part of the Guayuta group from which in some locali-
ties it has been separated into the Querecual formation. It readily
correlates with a lithologically similar Middle Cretaceous horizon
in Colombia, Ecuador, Peru, and Argentina.

Topographic expression and local details —Although the lower
portion of La Luna formation on Rio Cachirt contains resistant
beds of limestone, their total thickness is so slight in comparison

301 Rio Cacuiri SECTION: LIDDLE 30

with the underlying Cogollo formation, that they have no marked
influence on topography. The upper and more shaly portion of
La Luna breaks down readily, and the resultant low relief grades
imperceptibly into the narrow valleys which are underlain by
shales of the overlying upper part of the Guayuta group.

On Rio La Luna, however, resistant limestones range so much
higher in the section than in other places that the entire La Luna
formation sustains rugged, fairly high mountains through which
the river has cut a steep-walled channel.

Sample 50 was collected from La Luna formation on Rio
Cachiri.

Guayuta Shale

Name.—The Guayuta formation was introduced in 1928 by
Liddle’® and in it he included what is now known in the eastern
part of Venezuela, from base to top, as the Querecual, San An-
tonio, and the Santa Anita (lower part) formations,—the term
Guayuta being retained as a group name to include all three for-
mations. In the western part of Venezuela, in Sierra de Perija,
the same section is now designated, from base to top, as La Luna
formation, Guayuta shale, Colon formation, and Mito Juan for-
mation.

Stratigraphic position.—On Rio Cachiri the Guayuta shales are
perfectly conformable on shales and limestones of La Luna for-
mation; in fact the relation is almost a gradation. It is difficult
to determine where the top of La Luna formation terminates and
where the Guayuta shale begins because this part of La Luna is
predominantly shale containing some thin limestone beds, and
the basal Guayuta is made up of similar shale with almost no
limestones. Furthermore, it is not known for certain if the steep-
ly inclined, nodular, grayish-black shales which lie beneath the
Rio Guasare formation with seeming unconformity are the uppér
part of the Guayuta or if they should be placed in the Colon for-
mation. There is an interval on Rio Cachiri directly below the
Rkio Guasare formation which is concealed by detrital and in this

16 Jiddle, R. A.: op. cit., p. 154 ff.

34: BULLETIN 108 302

interval, that is apparently underlain by shale, the Colon forma-
tion may be present.

Physical character.—Dark-gray to erayish-black, calcareous
shales similar to those in La Luna formation comprise the basal
part of the Guayuta shale section, These grade upward into gray-
ish-black, nodular shales that are brittle when dry and unctuous
when wet. There is very litttle sand but not infrequent thin seams
of clay-ironstone. Upward in the Guayuta the shales become
lighter gray, fracture readily, and contain 1o-foot ledges of com-
pact, dark-gray, micaceous shale that is slightly calcareous.

Extent and thickness —There are about 1,800 to 1,900 feet of
Guayuta shale exposed on Rio Cachiri. Heavy forests which
conceal much of the outcrop render accurate measurements im-
possible. Furthermore, the dip is so steep that a slight change
in rate in concealed areas would materially affect the results ob-
tained. The Guayuta shale occurs in a narrow zone throughout
the length of the Sierra de Perija, but it varies widely in thick-
ness from place to place because of faulting and possible uncon-
formity at its top.

Age and correlation—Megascopic fossils are rare in the Guay-
uta shale, and in the northern part of the Sierra de Perija no
microscopic study of the formation has been made. However,
the upper part of the fossiliferous La Luna formation below, into
which the Guayuta shale grades, is definitely fixed as Lower
Cenomanien; consequently, the Guayuta shale is believed to be
Upper Cenomanien and in part Turonien.

Topographic expression and local details —Relatively low val-
leys mark the outcrop of the Guayuta shale in the Sierra de
Perija. It weathers rapidly, but where a bluff remains its face
is usually scarred by landslides. The greater resistance of the
Cogollo and the basal part of La Luna formations to the west,
and the Rio Guasare and Misoa-Trujillo formations to the east,
make valleys occupied on Rio Cachiri by the Guayuta shale and
the upper, more shaly part of La Luna formation fairly conspic-
uous.

Sample OI-J-146-++-20 is from La Luna formation.

|

303 Rio Cacnirt Section: LImDpLEe 3e

THE CRETACEOUS-EOCENE RELATIONSHIP

The soft, poorly exposed shales of the Upper Cretaceous on
Rio Cachiri do not afford reliable observations of dip for com-
parison with the fairly steep, eastward dipping Rio Guasare for-
mation of basal Eocene age. However, a short distance to the
west of the outcropping limestones of the Rio Guasare forma-
tion that dip eastward at 60° are Upper Cretaceous shales which’
are highly inclined eastward, or are vertical. Some of this dis-
turbance may be due to a strike fault observed in this horizon
farther south in the Sierra de Perija and suspected to be present
on Rio Cachiri where the Upper Cretaceous section is thin.

CENOZzOIC

Cenozoic sediments in the Sierra de Perija on Rio Cachiri in-
clude only the lower Eocene. Unconformably on the Upper Cre-
taceous hes the Rio Guasare formation, a glauconitic, calcitic,
reef-limestone of Midwayan age. It grades upward into the
Third Coal horizon which constitutes the lower member of the
Misoa-Trujillo formation, and is lower Eocene in age. The
eastern foothills of the Sierra de Perija, on Rio Cachiri, are made
up of hard, sandy, lignitic shales and thinly bedded sandstones of
the Third Coal horizon. This horizon extends eastward into
the Inciarte coal basin, and seems to have an erosional unconform-
ity marking its upper level, and to be unconformably overlain
by Oligocene sandstones and sandy shales. It would not be sur-
prising if this horizon of the Oligocene rests unconformably on
the Third Coal horizon along most of the eastern foothills of the
Sierra de Perija, having overlapped the truncated edges of the
intervening beds not removed by middle and upper Eocene
erosion.

Lower Eocene

Rio Guasare Formation

Name.—Garner™ in 1926 applied the name Rio Guasare for-
mation to basal Eocene limestones that are well exposed on Rio
Guasare above the Guayuta shale, in which may be included part

a7 Garner, A. H.: loc. cit.

36 BULLETIN 108 304

or all of the Colon formation, of Upper Cretaceous age and be-
low the Third Coal horizon of lower Eocene age.

Stratigraphic position—On Rio Guasare the well-developed
Rio Guasare formation, dipping eastward at 60°, lies on highly
inclined to vertical shales of the Upper Cretaceous. Heavy for-
ests, and detrital from the surrounding mountains conceal the
actual contact, but the nearest exposures of the two formations
have wide variation in dip. There is complete conformity be-
tween the Rio Guasare formation and the overlying Third Coal
horizon which is also lower Eocene in age.

Physical character.—The Rio Guasare formation on io
Cachiri, where the best exposures in the Sierra de Perija are to
be found, is a typical, impure, glauconitic, reef-limestone contain-
ing beds which are masses of closely packed oyster remains. The
limestone is so hard and the shells so calcitized that identifiable
specimens are difficult to extract. On weathering the glauconite
makes red splotches over the grayish-yellow surface of the lime-
stone. The individual beds of the limestone are regular and vary
from three to four feet in thickness.

Extent and thickness —On Rio Cachiri the Rio Guasare for-
mation is from 350 to 1,000 feet thick depending upon where the
contact with the overlying Third Coal horizon is placed. There
are 350 feet of solid limestone which introduces the Eocene, but
thin limestone beds, identical in character with the basal beds,
occur at various levels upward through 1,000 feet of sediments
which some place in the Third Coal horizon. The Rio Guasare
formation of basal Eocene age, though variable in thickness over
Venezuela and Trinidad, as would be expected from its charac-
ter and nature of deposition, has wide distribution, It occurs in
many localities in the eastern edge of the Sierra de Perija, is ex-
posed again on Rio Cachiri farther downstream at the eastern
edge of the Inciarte coal basin where it reaches the surface in
association with Cretaceous sediments, forms small outcrops on
Isla Toas, reaches the surface at several localities across Vene-
zuela, forms much of Isla Soldado in the Gulf of Paria between
Venezuela and Trinidad, and has been uncovered in Marac

305 Rio Cacuirt Section: LIDDLE 37

Quarry on the Island of Trinidad. It also outcrops on Arroyo
Cerrejon in the valley of Rio Rancheria, Department of Magda-
lena, Colombia where it is known as the Arroyo Cerrejon lime-
stone.

The Rio Guasare formation is thicker on Rio Cachiri than it
is at any other place yet known in Venezuela, However, the sec-
tion in Marac Quarry on the Island of Trinidad may be as thick.

Age and correlation —Turritella mortont Conrad, Turritella
negritosensis Wood, Venericardia planicosta Lamarck, Ostrea
bellovacina Lamarck, Ostrea selleformis Conrad, and Calyptra-
phorous trinodiferus Conrad from the Rio Guasare formation in-
dicate its lower Eocene age. Its unique physical character and
fossil content readily identify the formation either on the surface
or in the subsurface.

Topographic expression and local details —The hard limestone
beds of the Rio Guasare formation make prominent ledges in Rio
Cachiri just east of the topographically low area occupied by soft
shales of Upper Cretaceous age, but the thickness of the forma-
tion is not sufficient to give it much effect on general topography.

Sample OI-J-142+30 is from the Rio Guasare formation.

Misoa-Trujillo Formation: Third Coal Horizon

Name.—Liddle'® in 1928 wrote:

The Misoa-Trujillo formation receives its name from the Serrania de
Trujillo and a spur of this range, called Sierra Misoa, both of which have
a general northerly trend through the eastern parts of the districts of
Sucre and Bolivar, State of Zulia. Over practically all parts of Venezuela
where this formation, or its equivalents, is exposed two more or less dis-
tinct members are recognizable, though in all places they are not mappable
divisions. These members, from below to above, are the Third Coal horizon
PING! WN) Gls Me lonola Ge sandstone. The Third Coal horizon is so firmly estab-
lished in the nomenclature of western Venezuela that it is impracticable
to ignore it or apply a new name. It was first used in the District of
Colon, where it is the oldest of three coal-bearing horizons, the other two
being in the Oligocene and Miocene.

Hedberg and Sass’® in 1937 applied the name Paso Diablo for-
mation to at least a part of the Third Coal horizon where it out-
crops in Cano El Paso del Diablo, a tributary of Rio Guasare
about 25 kilometers north of Rio Cachiri.

18 Taddle, R. A., op. cit., p. 181.
19 Hedberg, H. D. and Sass, L. C., op. cit., pp. 95-96.

38 BuLLETIN 108 306

Stratigraphic position.—Vhe Third Coal horizon of the Misoa-
Trujillo formation les with perfect, and gradational conformity
on the Rio Guasare formation. The contact is beautifully ex-
posed in the banks of Rio Cachiri where massive limestones total-
ing 350 feet grade upward into sandy, carbonaceous shales and
sandstones that carry beds of coal. The contact of the Third
Coal horizon with the overlying sandstones and shales of Oligo-
cene age occurs several kilometers east of the foothills of the
Sierra de Perija in the center of the geosynclinal coal basin which
lies between the mountains on the west and Cerro Los Guineos on
the east. These overlying sandstones and shales are considered
to be Oligocene in age, and they transgress the eroded edges of
the Third Coal horizon,—the unconformity between representing
a great erosional interval.

Physical character.—Massive, and thinly bedded, fairly hard,
grayish-brown, micaceous, locally calcareous sandstones inter-
calated with gray, sandy, micaceous shales containing scattered
lignite and beds of sub-bituminous to bituminous coal which vary
from a few inches to 30 feet in thickness comprise the Third Coal
horizon. Large exposures of the thinly bedded sandstones and
shales in the channel of Rio Cachiri have beautiful, regular ripple
marks. Layers and isolated concretions of clay-ironstone are
common.

Extent and thickness—TYhe Third Coal horizon occupies a
wide belt in and to the east of the Sierra de Perija on Rio Cachiri.
It forms the foothills of the mountains, and extends eastward in
the shallow geosyncline which reaches to Cerro Los Guineos.

Northward from Rio Cachiri it also makes up the foothills and
the western rim of, as well as underlies, the geosyncline just re-
ferred to. Southward from Rio Cachiri it forms much of the
eastern edge of the Sierra de Perija but in places part of the
horizon is truncated and overlapped by massive sandstones and
shales of Oligocene age which comprise some of the foothills belt.

An estimated thickness of at least 3,000 feet of the Third Coal
horizon is exposed on Rio Cachiri. Faulting of unknown magni-
tude renders accurate measurements impossible. There is some

307 Rro Cacuirt SECTION: LIDDLE 39

suggestion that the Third Coal horizon may reach an excessive
thickness in this area,

Age and correlation No fossils have been found in the Third
Coal horizon, but its close relation to the Rio Guasare formation
below, whose lower Eocene age is positive, indicates that it too is
lower Eocene. This lower Eocene horizon has wide distribution
over Venezuela, is consistently coal-bearing, and in places fur-
nishes valuable mines of coal.

Topographic expression and local details —Rugged foothills
in the eastern edge of the Sierra de Perija are formed by the
Third Coal horizon. On Rio Cachiri, where the river cuts through
the eastern edge of the mountains, thinly bedded sandstones and
intercalated sandy, coal-bearing shales form a gorge at the head
of Playa La India.

Rocks exposed.on Rio Cachiri, between the core of the
Sierra de Perija on the west and the foothills of the mountains
on the east, if minor structural disturbances are disregarded,
form the eastward dipping flank of a great anticline whose
axis trends north-south. Excepting local irregularities, some
of which have considerable magnitude, there is a decrease
in dip eastward from the axis of the anticline which coincides with
the core of the mountains. This core is part of an old, deeply
rooted land mass of probable Archeozoic age which has been
called the Sierra de Perija mass.?°.

Viarious periods of movement and intervals of erosion have oc-
curred while these mountains were reaching their present form.
Uplifts of magnitude, followed by marked erosion, took place
between Archeozoic and Devonian, Devonian and Permo-Car-
boniferous, Permo-Carboniferous and Cretaceous, Cretaceous and
Eocene, during middle and upper Eocene, and in the Miocene
when the major Andean uplift occurred. Faulting and igneous
activity accompanied some of these disturbances.

20 Liddle, R. A., op. cit., pp. 364-365.

40 BULLETIN 108 308

DESCRIPTION OF SAMPLES FROM RIO CACHIRI

Localities of samples indicated on the accompanying map by
numbers inside circles. All specimens are on file in the labora-
tory of the Paleontological Research Institution.

Samples from the Caio del Norte branch of Rio Cachivi

Sample ‘‘A’’.—Quartz syenite or aplite and quartz diorite having pink
and green splotches on a mottled grayish-rose ground-
mass of pink feldspar and dense, amorphous silica in
which are embedded transparent, glassy quartz erystals.
There are some specks of hornblende, and a trace of iron.

Sample ‘‘B’’.—Dark-gray, dense limestone extremely shattered and con-
taining veins and angular pockets of calcite. Both the
limestone and the calcite are slickensided in places.
Permo-Carboniferous, intruded by diorite.

Sample ‘‘C’’,—Dark-gray, hard, fine-grained sandstone formed by small,
angular, and round quartz grains cemented together with
a slight amount of calcite, and having much dark green-
ish-black mineral resembling hornblende and some tiny
fragments of ferruginuous matter. The rock appears
to have been derived from an igneous or metamorphic
source although it lacks mica which is present in quan-
tity in most of the igneous, sedimentary and metamor-
phie rocks of the region. Upper Devonian.

Sample ‘‘D’’.—Deep-red, shattery-fracturing, unctuous, compact shales
having greenish-white splotches. The matrix is fine, red
silt that contains tiny particles of ferruginous matter.
The shale is non-caleareous and unfossiliferous. Permo-
Carboniferous.

Sample ‘‘E’’.—Same as Sample ‘‘D’’.

Sample ‘‘F’’.—Dark grayish-black, crinoidal limestone composed chief-
ly of ealcitized crinoid roots, and stems ranging from
one millimeter to one and. one-half centimeters i
diameter. The original rock and the replacement min-
erals are definitely slickensided. One rock fragment
contains the hinge area of a fairly large Spirifer whieh
indicates its Paleozoic age, and a large, tubular Bryozoa.
These fossils might indicate Devonian age, sinee they
are associated in Devonian shales farther west on Rio
Cachiri and deeper in the stratigraphie section, but the
small percentage of limestone in the Devonian raises
considerable doubt about such a correlation. Further-
more, in order to reach its present position the erinoidal
limestone, were it of Devonian age, would have to have
been carried by the associated igneous intrusion through
much Upper Devonian section and entirely through the
red-bed section at the top of which the crinoidal lime-
stone lies. It seems more probable that the erinoidal

309

Rio Cacutri SEcTION: LIDDLE 41

limestone is practically in its normal position in the
stratigraphic section at the top of the red beds, and
below the Rio Negro formation of basal Cretaceous age,
and that its absence on other branches of Rio Cachiri
is due to the great unconformity which exists at its level
between the red-bed section below and the basal Creta-
ceous above. It is doubtful if the intrusion with which
the crinoidal limestone is associated could have carried
it up from the fossiliferous Lower and Middle Devonian
several thousand feet below. Lithologically the crinoidal
limestone does not resemble any Devonian beds seen in
the region. Sample ‘‘F’’, like Samples 15 and 16, is
abnormally heavy because of impregnation by iron.
However, Samples 15 and 16, especially 16, are more
reddish than black, either from original coloring or from
ferruginous stain, because of their proximity to the
igneous intrusion (Sample ‘‘A’’). Permo-Carbonifer-
ous.

Sample 1.—Dense, dark-gray, sandy limestone slightly altered and cut

by calcite veins; dense, dark, fine-grained, slightly mica-
ceous, calcareous sandstone which carries small flakes
of biotite. It is shattered and cut by calcite veins, and
its weight suggests impregnation with iron. The De-
vonian at this locality forms a narrow gorge with over-
hanging walls. Steep slopes of the mountain sides de-
scend to the rim of the gorge-so that in order to con-
tinue upstream a trail must be cut high up on the moun-
tain side. This was done by the 1924 expedition which
collected fossiliferous Lower and Middle Devonian two
kilometers upstream from the gorge. No metamorphic
or igneous float was found in the Cano del Norte branch
of Rio Cachiri so it is doubtful if this branch reaches
the core of the mountains. For this reason more time
was spent on the other branches of the river, which,
judging from their westerly course, had more chance to
cut to the core of the mountains. Upper Devonian.

Sample 2—Identical in character with Sample 1, and with Sample

Sample 3.—Dense, greenish-black diorite,

SPeLeMMg Ne) pn Ae

OI-J-72. Upper Devonian.

the same as Sample 5
and Sample OI-J-69.
Same as Sample 3.

S
Sample 5—Dense, greenish-black diorite.
Sample 6.—Very deep red, highly micaceous, sandy shale which has

a blocky fracture. Its weight suggests impregnation
with iron. Permo-Carboniferous.

Sample 7.—Same as Sample 6.

Sample OI-J-63

3.—Reddish and greenish quartz syenite or aplite and
quartz diorite which have intruded and altered the as-
sociated red shales. Angular fragments of greenish-
black igneous rock are present in the reddish ground-
mass. There is much clear quartz, and veins of eal-
cite traverse the rock where it is fractured. Sample

BuLLETIN 108 310

OI-J-63 resembles Sample ‘‘A’’ to some extent; how-
ever, in Sample ‘‘A’’ the rock is homogeneous and
aphanitic whereas in Sample OI-J-63 quartz crystals
and greenstone fragments are common. Some parts
of Sample OI-J-63 resemble igneous breccia im that
it contains fragments of basalt one centimeter in di-
ameter. Sample 8 is from same outcrop. }
Sample 9.—Highly micaceous, dark-gray, sandy shale and highly
micaceous deep-red shale. The red shale is similar to
Samples 10, ‘‘D’’, and ‘‘ E’’ but has more mica. There
are neither megascopic nor microscopic fossils. Permo-
Carboniferous.

ample 10.—Deep-red, hard, shattery-fracturing shale having green-
ish-white splotches and earrying tiny flakes of mica. Not
fossiliferous. Identical in character with Samples ‘‘D”’
and ‘‘E’’. Permo-Carboniferous.

Sample 11.—Same as Sample 10.

Sample 12.—Identical with Samples ‘‘B’’ and 13.

Sample 13.—Identical with Samples ‘‘B’’ and 12.

Sample 14.—A large bluff in the west bank of Cafio del Norte com-
posed of pinkish-gray aplite resembling the limestone
which it has intruded; dense, hard, gray, unfossiliferous
limestone containing no ealeite; and pink to reddish,
erystalline limestone that is full of calcite crystals. Both
types of limestone appear in the same ledge, are unfos-
siliferous, and have the appearance of being slightly
altered. Permo-Carboniferous, and igneous.

Sample 15.—Dark-gray to reddish-gray and red, crinoidal limestone
similar to Sample 16. It contains a large, remose form
similar to Rhombopora or Alveolites; the hinge area
of a fairly large Spirifer; and a few Teaxtularia-
like Foraminifera which occur in some pieces of the
dense limestone and are visible in thin-sections. Permo-
Carboniferous.

Reddish-black to black and red, erinoidal limestone in which

crinoid remains comprise 50 per cent of the rock. There

are many crinoid roots, and the abundant stems vary from
one millimeter to one and one-half centimeters in diam-
eter. All of the remains are replaced by calcite. The rock
is unusually heavy because of impregnation with iron. It
weathers gray. This crinoidal limestone lies with seeming
unconformity, although the actual contact is concealed, be-
low the Rio Negro formation of basal Cretaceous age. On
its northwest this limestone is in contact, in the river bank,
with the quartz syenite and quartz diorite of Sample ‘‘A’’.
In the southwestern bank of the river the erinoidal lime-
stone grades into a large bluff (Sample 14) of massive,
reddish-black and black crystalline limestone intruded by
aplite. The limestone lacks erinoid remains, and weathers
pitted and cavernous. Farther northwest the massive lime-
stone bluff appears to be in normal contact with the red-
bed section that separates it from the Devonian.

M

Sample 16.—

Evidence

et

Sample

Sample

Sample

Sample

Sample

Sample

Sample

Sample

Rio CacHirI SEcTION: LippLE 43

at present, although not final, indicates that the crinoidal
limestone and the unfossiliferous, crystalline limestone are
parts of the same deposition, as is the red-bed section. All
are believed to be Permo-Carboniferous,—probably Perm-
ian. To date no fossils of any sort have been found in
these beds. The crystalline character of some of the lime-
stone is doubtless due to its proximity to the aplite intru-
sion. This intrusion contains almost no iron and is appar-
ently not the source of the iron in some of the nearby lme-
stones. They may have been enriched by waters and vapo.s
ascending along the contact. This aplite mass is complemen-
tary to the basalt dikes to the west and northwest.

17.— Quartz syenite or aplite and quartz diorite composed of
quartz, feldspar, and a small amount of iron. In weather-
ing some of the outer edges of the mass resemble sand-
stone, the quartz crystals standing out above the flakes of
feldspar which are irregular-shaped white flecks.
Samples from the Cano del Oeste branch of Rio Cachiri

18.—Identieal with Samples ‘‘D’’ and ‘‘E’’ in lithologic char-
aeter, but the shale at Sample 18 is twisted, shattered, and
erumpled by folding and faulting. Permo-Carboniferous.

19.—Dark-gray, dense, fine-grained, quartzitic sandstone com-
posed of small, rounded and angular grains of quartz. There
is considerable dark-green mineral resembling hornblende.
The rock appears to have been derived from igneous ma-
terial, but it has no mica. It is identical with Sample
“°C??. Upper Devonian.

20.—*A’?: Quartzite composed of well-rounded, clear, fairly
large quartz grains held together by siliceous cement. There
is a slight amount of ferruginous matter.
‘“B’’:Quartzite composed of rounded, very small quartz
grains held together by siliceous cement. In places the
quartz crystals appear to be fused. Upper Devonian.

21.—Highly micaceous, questionably lignitic, irregularly bedded,
limonitic, grayish-brown shale which is fairly well com-
pressed. It appears to have been laid down in shallow
water, as it is interbedded with thin, quartzitic layers.
Upper Devonian.

22.—Gray, slightly calcitic, micaceous, hard quartzite composed
almost entirely of interlocking, clear quartz crystals. There
are a few black specks, and an occasional green one which
may be hornblende, in addition to much mica. The outerop
forms a massive bluff in which the thinner layers are evenly
bedded. Upper Devonian.

23.—Dull-red shale containing some fine, clear quartz sand and
much mica. Permo-Carboniferous.

OI-J-97.—Deeply weathered, highly fossiliferous, ferruginous,

(Float ) gray clay shale containing much mica and some fine

sand. Fossils identified are:

Spirifer kingt Caster

Spirifer, sp. (fragments)
These fossils indicate Lower and Middle Devonian
age.

44.

Sample

Sample

Sample

Sample

Sample

Sample

Sample

Sample

BuLuETIN 108 312

24.—Brown, quartzitie sandstone containing many particles of
hematite and white flecks which are probably weathered
feldspar. The quartz grains are fairly rounded. This fer-
ruginous, quartzitic sandstone resembles parts of the
Imataca series. Upper Devonian.

25.—Grayish-brown, micaceous, limonitie shale which shows ne
it has been fairly well pressed. It is similar to Sample 21
in character but is much more evenly bedded. Upper De-
vonian. ; a

26.—Grayish-brown, fine-grained, ferrugimous, quartzitic sand-
stone. The quartz grains are fairly well rounded and quite
small. Highly limonitic and resembles parts of the Imatacé
series. Upper Devonian. a

27.—Gray, evenly bedded, highly micaceous, quartzitie sandstone.
The erystals of quartz are very small and among them are
scattered small, dark specks resembling hornblende. Some
beds are massive; others are thin. Upper Devonian.

28.—Deep-red, greenish-gray, splotched, micaceous shale. Iden-
tical with Samples ‘‘D’’, ‘‘E’’, 10, and 18. It immediately
and conformably underlies the quartzitic sandstone of Sam-
ple 27 whereas in normal sequence it should overlie the
sandstone. Permo-Carboniferous.

29.—Reddish-brown, dense, very fine-grained, silty sandstone. The
quartz grains which make up the bulk of the rock are very
small. This sandstone, like the shale above it (Sample 28),
is not in normal position in the section. Permo-Carbon-
iferous.

30.—Fairly soft, light-brown, white-flecked, medium coarse,
quartzitie sandstone in which the quartz grains although
variable in size are well rounded. The white flecks are
weathered feldspar. There is a little ferruginous matter.
Upper Devonian?
In the lower part of Cafio del Oeste some portions of the
red-bed section of the Permo-Carboniferous and some beds
of the Upper Devonian are interposed. This is noticeable
between the localities of Samples 18 to 31. It may account
for our inability to find the conglomerate which marks the
base of the Permo-Carboniferous and its contact with the
Devonian on Cano Grande. A great amount of faulting
has occurred between the localities of Samples 18 and 31.
Not only have Upper Devonian and Permo-Carboniferous
rocks been interposed but the rocks themselves are indur-
ated, and well-developed slickensides exist in the shales and
even in the quartzitie sandstones. Older beds in the De-
vonian show little evidence of such intense disturbanee, and
no evidence of induration by compression.

31.—Gray shale containing very little mica,
with limonite.
less mica.
Devonian.

: and stained brown
+88
Similar to Samples 21 and 25 but

having:
3 >
The beds are vertical and overturned.

Upper

S; ~ page es say's ee -
ample OI-J-113. Brown, soft, highly micaceous, very sandy, clay shale
(Float) containing :

B Rio Cacwirt Srction: LIDDLE 45

' Kdmondia sylvana Hartt
Leptodomus ulrichi Clarke

/Nucula?, sp.

¥ Tellinopsis venezuelana, n. sp.

? Productus liddlei, n. sp.

Schellwienella goldringe Caster

The character of the material composing the several
fragments of this sample is very uniform but the
fossils indicate that both Devonian and Carbonifer-
ous are represented. The Producti suggest Carbon-
iferous whereas the other fossils are Devonian. No
sediments in place, in the Permo-Carboniferous sec-
tion which lies between the Devonian and the Cre-
taceous on Rio Cachiri, bear any resemblance to this
Carboniferous float. Its source, though, must be in
the watershed of this river which is relatively small.
Careful search of the upper reaches of other rivers
in this part of the Sierra de Perijé may reveal a
more complete Carboniferous section than is now
known. Fusulina from the upper course of Rio
Palmar indicate the presence there of Carboniferous
rocks not yet found in Rio Cachiri. Both Devonian
and Carboniferous are represented in this sample.

Sample 31.—-Grayish-black limestone containing some small erinoids that

(Float) are replaced by calcite. Fossils identified are:
Fenestella venezuelensis Weisbord
Spirifer, sp.
Lower and Middle Devonian.

Sample 52.—Grayish, ferruginous, highly micaceous, compact sandy shale
containing small, dark specks like hornblende. Sample 382
is 50 feet upstream from Sample 31. Upper Devonian.

Sample 33.—Hard, dark-gray, micaceous shale which is well bedded and
full of very small flakes of mica. It contains no fossils but
has caleareous concretions. Upper Devonian.

Sample 54.—Gray, micaceous, sandy shale which is highly weathered and

(Float) stained brown in places by limonite. Fossils identified are:
Polypora cachirita Weisbord
: Rhipidomella liddlei, n. sp.
Strophonella? meridionalis (Caster)
Lower and Middle Devonian.

Sample 35.—Same in character as Sample 33 but showing well-developed
slip-planes due to squeezing. The shale is standing vertical.
Not fossiliferous. Upper Devonian.

Sample 36.—Dark-gray, fossiliferous shale. Fossils identified are:

(Float) Heliophyllum halli Mine Edwards and Haime
-Heterophrentis venezuelense (Weisbord)
Lower and Middle Devonian.

Sample 37.—Dark-gray, fossiliferous, caleareous shale and shaly lime-
stone containing a few calcite crystals. It forms a deep,
narrow gorge with one overhanging wall. There are many
corals and some crinoid stems. Fossils identified are:

BULLETIN 108 314

Heliophyllum halli Milne Edwards and Haime
Heterophrentis venezuclense (Weisbord)
Lower and Middle Devonian.

Sample 38.—Grayish, highly weathered, limonite stained, fossiliferous,
(Float ) calcareous shale or shaly limestone. Many of the fossils are

Sample

Sample

Sample

Sample

Sample

casts filled with powdery limonite. Fossils identified are:
, Fenestella venezuelensis Weisbord
‘ Atrypa reticularis var. harrisi Caster
Elytha? plana, 1. sp.
Lower and Middle Devonian. :
39.—Gray, sandy, unfossiliferous, concretionary shale with infil-
tration and metalic stain from oxide of manganese, In
this sample the stain is like burnished copper, whereas in
other samples it has an irridescent purplish-black color.
There are microscopic particles of lignite. Lower and Mid-
dle Devonian.
40.—Grayish-brown, micaceous, sandy clay carrying many clay
pellets that are stained by limonite. These sediments ap-
pear to be shallow water deposits similar to Samples 21, 25,
and 31. They contain very little mica. Lower and Middle
Devonian.
41.—Dense, black, unctuous clay shale -which is extremely twist-
ed and contains many slip-planes. There is little mica, and
the shale has a decidedly nodular character. Much of the
exposed section is vertical. Lower and Middle Devonian.
42.—Gray, ealeareous shale and darker gray shaly limestone and
shale. The dark shales have well-developed slip-planes and
show compression. At the localities of Samples 42 and 45
the outeropping beds are highly fossiliferous but the shale,
and especially the black limestone, are so hard that the fos-
sils can be extracted only where the rocks are extremely
weatherd. Fossils identified are:
Fenestella venezuelensis Weisbord
Polypora cachirita Weisbord
Platyceras gibraltar, n. sp.
- Spirifer, sp.
?Aviculopecten yeakeli Weisbord
Many fragments of corals and erinoids
Lower and Middle Devonian.
45.—Deeply weathered, dark-gray and light-gray shale in which
the body cavities of fossils are filled with powdered limon-
ite. The shale is highly fossiliferous. Fossils identified
are:
Fenestella venezuelensis Weisbord
Polypora cachirita Weisbord
.Pecten, sp. (fragment)
> Acrospirifer olssoni Caster
Lower and Middle Devonian.

Rio Cacuiri Section: LippLEe AT

Sample 44.—Grayish, pink- and brown-stained, schistose, igneous quartz

from a large boulder which blocks the narrow gorge of the
river at this locality. The boulder is 30 feet in diameter
and evidently has not been moved far, except possibly to
roll down a steep mountain side. It is not possible to pass
this place except by cutting a trail and climbing around the
mountain side. There was not time for this. The boulder
is from the Sierra de Perijé series of probable Archeozoie
age.

There are many large quartz boulders and a number of
smaller granite blocks in the river at this locality. Much
of the granite is schistose, light in color, and contains much
mica. The schist boulders and fragments are smaller than
those of granite and quartz. These igneous and metamor-
phie rocks comprise much more of the stream detrital than
do the Devonian sediments which form the walls of the ean-
yon at this locality. It is believed that the base of the
sedimentary section is not far upstream. At the locality
of Sample 44 the Cano del Oeste branch of Rio Cachiri has
decreased to about one-fourth of its size at Campo Las Dos
Boeas. The water in the narrow channel averaged four feet
in width and six inches in depth, except in a few deep
holes.

Samples from the Caio Grande branch of Rio Cachiri

Sample 50.—Black, petroliferous, highly fossiliferous limestone in which

the fossils are completely replaced by calcite. The sample
is typical of the ellipsoidal and discoidal limestone masses
embedded in black carbonaceous shale. These masses ap-
pear to have been formed in pockets or depressions in the
sea floor in which calcium carbonate, possibly from the
tests of fossils, accumulated while around them silt and
mud were being laid down. The bed from which the sam-
ple was collected is a part of a La Luna formation which
hes conformably between Guayuta shale above and Cogollo
limestone below. The age is Middle Cretaceous or Vracon-
nien. The locality of the sample is at the downstream en-
trance to a boulder-choked gorge of Cogollo limestone whose
walls rise 400 feet vertically above the river bed. The
Cogollo limestone is massively bedded, bluish gray in color,
weathers pitted or cavernous, and on exposed surfaces are
many calcitized rudistids, Ostrea, sp., and Trigonia, sp.,
which show in cross-section but which can not be extracted.
There is little evidence of the Rio Negro formation of basal
Cretaceous age on Cano Grande. Beneath (upstream from).
the outcrop of the Cogollo limestone is a narrow, debris-
filled valley, and the first reliable outerop (Sample 51) is
red, brittle, micaceous shale. A few massive boulders of
brown, fine to coarse, conglomeratic sandstone occurring
just below the outcrop of the Cogollo limestone indicate
the presence of the Rio Negro formation.

Sample

Sample

Sample

Sample

Sample

Da

BULLETIN 108 316

In Cafio Grande, shale of the Guayuta is exposed for the
first kilometer above its junction with the other part of
Rio Cachiri. The shale underlies a low valley, but ex-
posures are frequent enough in the river bed and banks to

show

that the shale is grayish black, nodular, coneretion-

ary, has a shattery fracture, and is standing vertical. In
its lower part the nodular, gray, concretionary clay shale
changes gradually into thinly bedded, black, petroliferous
limestone and intercalated black shale in which are em-
bedded ellipsoidal and discoidal, black, petroliferous lme-

stone

bodies. There are, also, thin bands of black chert.

Where shattered, the limestone is eut by veins of white
calcite.

51.—Well-bedded, micaceous, dull-red, brittle, unfossiliferous,
sandy shale which is slightly lignitie. Sample 51 was col-
lected one kilometer upstream from the base of the Cogollo
limestone outcrop. The shale contains no megascopic or
microscopic fossils. Permo-Carboniferous.
52.—Conglomerate having a matrix of deep, dull-red, micaceous,
sandy shale in which are embedded large, angular fragments
of light- and dark-gray limestone. The original gray of the
limestone has in places been stained red with iron derived

from
mueh

the shale portion of the conglomerate which contains
ferruginous matter. There is a continuous exposure

of red shale from the locality of Sample 51 to that of Sam-
ple 52. Permo-Carboniferous.

ONS

Micaceous, ferruginous, dull-red shale which is
nodular in character and appears to have been de-
posited in shallow water. Like Sample 52 the shale
contains fragments of gray limestone. Sample 53
‘A?? and Sample 52 are a conglomeratie horizon
that marks the base of the red-bed section. Permo-
Carboniferous.

‘“B’?: Gray, micaceous, very arenaceous, limonite-stained

shale containing much finely disseminated lignitic¢
matter that apparently was derived from leaf frag-
ments. , Interealated with the evenly bedded shales
are bluish-black, ferruginous, fine-grained, quartzitic
sandstone. The ‘‘B’’ portion of the sample is con-
sidered to be the top of the Devonian section and is
here referred to the Campo Chico formation, and cor-
related with the Rio Macoita formation. Upper De-
vonian.

54.—Dark bluish-gray, fine-grained, ferruginous, quartzitie sand-

stone
with
lying

vonian.

shattered in places and having the fractures filled
caleite. Closely resembles the quartzitic sandstones
below the red beds on Cano del Oeste. Upper De-

55.—Gray, micaceous, thinly bedded, hard, sandy shale with
which is interealated hard, quartzitic sandstone that is shat-

tered

and has its fractures filled with calcite. The outerop

7 Rio CAcHtIrRI SECTION: LIDDLE 49

is continuous from the locality of Sample 54 to the loeality
of Sample 55. Upper Devonian.

Sample 56.—Dark bluish-gray, fine-grained, ferruginous, quartzitic sand-
stone more thickly bedded than Sample 55. Continuous out-
crop from locality of Sample 55 to locality of Sample 56.
Upper Devonian.
Thickly bedded, gray, nodular shale weathering brownish-
eray from ferruginous matter. The shale is highly con-
eretionary and -breaks with a shattery fracture. There is
finely disseminated lignitic matter which appears to have
been derived from leaf fragments, but none ,are recogniz-
able in the lignitie flakes. Upper Devonian.

Sample 58.—Dark-gray, micaceous, nodular shale weathering brownish
and interbedded with black, micaceous, slaty shale. The
dark-gray shale contains finely disseminated lignitic matter
that appears to have been derived from leaf remains. Where
the shale is shattered there has been replacement by calcite.
Upper Devonian.

Sample 59.—Dark-gray, very dense, slaty shale which breaks with a
splintery fracture that has been developed by compression.
It is not micaceous, caleareous, or fossiliferous but has a
slightly baked appearance due to its proximity to the dior-
ite intrusion (Sample 61). In the bluffs formed by this
outerop, which are 100 feet high and over one kilometer
in extent, there are thin layers of clay-ironstone. Upper
Devonian.

Sample 60.—Identical with Sample 59 and Sample 61. Upper Devon.
ian, and basalt.

Sample 61.—Dense, fine, bluish-black basalt sill 30 feet thick whose
alternating thick and thin layers are evenly bedded and
earry black, irregularly shaped masses of quartz. This
igneous intrusion has followed the bedding of the sedi-
ments which it intrudes, its main effect being the baking
of the adjacent shales.

Sample 62.—Identical with Sample 59. Upper Devonian.

Sampie 62.—Gray, calcareous, micaceous, fossiliferous shale having a
shattery fracture and being hard enough to form vertical
bluffs 60 feet high. In weathering the shale becomes soft,
and the casts of fossils are filled with powdery limonite.
In places the shale is slightly nodular and contains finely
disseminated lgnitic particles that seem to have been de-
rived from leaf fragments. The entire deposit appears to
have been laid down in shallow water. Fossils identified
are:

Sample 5

Synaptophyllum vermetum (Weisbord)
Platystoma ventricosum (Conrad)
. Platystoma ventricosum var. permudum, n. var.
. Leptena boyaca Caster

- Spirifer olssoni Caster

Spirifer weisbordi, un. sp.

50 BULLETIN 108 318

Heliophyllum halli Mime Edwards and Haime
Heterophrentis venezuelense (Weisbord)
.Meristella wheeleri Caster
Crinoid stems
The coral, Synaptophyllum vermetum (Weisbord), measured
two feet in diameter. This fauna indicates Lower Devon-
ian——about the horizon of the Helderberg and Oriskany
of New York State. ;

Sample 64.—Identical in character with Sample 65. Fossils identified

are: d

Stropheodonta (Cymostrophia?) casteri, n. sp.
Crinoid stems

Lower and Middle Devonian.

Almost identical in character with Samples 63 and 64, ex-

cept that there are more mud pellets. Fossils identified are:

Heliophyllum halli Mime Edwards and Haime
Crinoid stems (abundant)
Fenestella venezuelensis Weisbord
Polypora cachirita Weisbord
Athyris spiriferoides (Waton)
Atrypa reticularis var. harrisi Caster
Camarotechia, sp.
Chonetes venezuelensis Weisbord
¥ Dalmanella ef. nettoana Rath
Dictrostrophia cooperi Caster
Elytha colombiana Caster
Kodevonaria subhemispherica Weisbord
vLeptena rhomboidalis (Wilckens)
Leptostrophia concinna (Morris and Sharpe)
- Pentagonia wnisulcata Hall
» Productella, sp.
-Rhipidomella liddlei, n. sp.
Schellwienella goldringe Caster
Stropheodonta kozlowskti Caster
/Tropidoleptus carinatus Conrad
Actinopteria subulrichi, n. sp.
Amphigenia elongata var. weisbordi, n. var.
_Ctenodonta?, sp.
Shark’s tooth

This fauna indicates Lower and Middle Devonian age,

ranging from the Helderbergian through the Oriskanian and

into the Hamiltonian.

Sample 66.—Grayish, nodular, micaceous, calcareous shale having a shat-
tery fracture and containing many fenestelloid Bryozoa
and erinoid stems, the latter being replaced by caleite.
This shale forms bluffs 100 feet high on the south bank
of the river. The only fossil identified is:

Fenestella venezuelensis Weisbord
Lower and Middle Devonian.

Sample 67.—Identical in character and containing practically the same
fauna as Sample 66. Forms a high bluff on the south side
of the river. Lower and Middle Devonian.

Sample 65.

319 # Rio CacHtrr SECTION: LIDDLE 51

Sample 68.—Identieal in character and fossil content with Samples 66
and 67. Lower and Middle Devonian.
Sample 69—Grayish, mieaceous, sandy, non-caleareous, nodular shale
containing minute lignitice matter probably derived from
*vagments of leaves. Fossils identified are:
Fenestella venezuelensis Weisbord
Polypora cachirita Weisbord
Chonetes stiibeli Ulrich
~Hodevonaria imperalis Caster
Eodevonaria subhemispherica Weisbord
Leptostrophia caribbeana Weisbord
Meristella wheeleri Caster
Meristella, sp.
> Spirifer, sp. (fragments)
’ Limoptera tenuis, n. sp.

Lower and Middle Devonian.
Sample 70.—Quite similar in physical character to Sample 69, but dif-
fers in having more powdery limonite, well-developed slick-
ensided surfaces, and in being nonfossiliferous. Weathers
into convex-coneave particles. At the locality of Sample
70 there is a erushed zone along a fault exposed in the
south bank of the river. Black limestone on the east side
of the fault is in contact with grayish-black, nodular shale
on the west side of the fault. The strike of the fault is
due north-south, and the angle of its dip is 85° west. The
dip on the east side of the fault is 38° N. 45° W. but no
reliable observation can be made of the dip in the crumpled
shale on the west side of the fault. The convex-coneave
weathering shale of Sample 70 on the west side of the fault
is believed to lie, when in normal position, above the fossilif-
erous, gray shale of Sample 69 but the fault has dropped it
west of its regular position. These beds are thought
to be Lower and Middle Devonian in age.
Sample 71.—Grayish-black, nodular, sandy, fossiliferous shale which
forms a vertical walled gorge from 10 to 20 feet wide and
from 100 to 200 feet high. The fossils, principally erinoid
stems and cup corals, lie in layers and protrude from
weathered surfaces. There are at least 500 feet of the
shale exposed in this gorge. Fossils identified are:
Heliophyllum halli Milne Edwards and Haime
Heterophrentis venezuelensis (Weisbord)
Crinoid stems

Lower and Middle Devonian.

Sample 72.—Grayish-black, micaceous, calcareous, sandy, thinly bedded,
fossiliferous shale forming the upper end of the gorge des-
eribed in Sample 71. The shale contains lenses and seams
of reddish-clay-ironstone. Interealated in the shale are
black, irregularly bedded limestone layers. Fossils eon-
tained in the shale lie in layers exposed along the walls

‘

Sample

Sample

Sample

Sample

Sample

Sample

Sample

2 oO
BULLETIN 108 320

of the gorge. They are almost exclusively corals and
erinoids. Fossils identified are:

Heterophrentis venezuelensis (Weisbord )

Heliophyllum halli Milne Edwards and Haime

Platyceras sinistrum, un. sp.

Crinoid stems averaging two centimeters in diam-
eter (abundant).

Rhipidomella liddlei, nu. sp.

Lower and Middle Devonian.

character same as Sample 72. Fossils identified

are:

’Heliophylium halli Milne Edwards and Haime
Heterophrentis venezuelensis (Weishord)
Zonophyllum, sp.

/Platyceras sinistrum, n. sp.

Lower and Middle Devonian.

74.—Similar in lithologie character to Sample 72 but not fossil-
iferous. Sample 74 was taken at a six-foot falls at the
head of a large iol of water. Lower and Middle Devonian.

75.—Gray, micaceous, nodular, irregularly bedded shale having
films of limonite along fractures. The shale forms a nar-
row gorge, and is not fossiliferous. Lower and Middle De-
vonian.

76.—Dense, evenly bedded, very fine-grained, dark-gray, mica-
ceous, quartzitie sandstone which is not fossiliferous. With
this quartzitic sandstone are intercalated a minor amount
of more shaly sandstones which, although just as hard as
the more massive sandstones, carry imprints of small and
medium-sized Spirifers and corals. The quartzitie sand-
stones of Sample 76 lie conformably under the dark-gray,
nodular shales of Sample 75. Between the stations at which
Samples 75 and 76 were collected the dark-gray, nodular
shale becomes extremely nodular, soft, and shattery in frac-
ture. Lower and Middle Devonian.

77.—The quartzitic sandstones of Sample 77 are similar to those
described in Sample 76, but they are interbedded with
coarse, fairly soft, extremely micaceous, dark-gray sand-
stones made up of moderately rounded, clear quartz grains,
large flakes of biotite, and small grains of hornblende. The
more shaly members carry imprints of fossils mentioned in
Sample 76, but they are impossible to extract because of
the hardness of the rock. Lower and Middle Devonian.

774%4.—Hard, dark-gray, slaty shale which is only 50 feet east

(downstream) from the quartzite, quartz, schist, and
granite of sae 78. There may be a fault between
the slaty shale of Sample 7714 and the metamorphie and
igneous rocks of Sample 78 whieh form the core of the
Sierra de Perija. Lower and Middle Devonian.

‘ately soft, mica-hornblende schist containing consid-

erable white siliceous material disseminated throughout the
rock, and some small, clear quartz grains.
granite aiceriele principally of feldspar and quartz. Sierra
de Perija series. Archeozoie.

Medium hard

orl Rio Cacntrt Sretion: Lrpp.e 53

Sample 79.—Gray, massive micaceous quartzite which is cut by thick

dikes of pure, vitreous quartz. Sierra de Perijé series.
Archeozoie.
At and upstream from the localities where Samples 78 and
79 were colleeted there are only igneous and metamorphic
rocks exposed in the stream in sitw or as float. A cursory
examination of contact zones where quartz dikes and veins
cut the older metamorphic and igneous rocks revealed no
evidence of mineralization. However, a far more thorough
examination must be made before an unqualified statement
‘an be made.

=‘ “ie —

mn we ie > :
ane ial Me

ee

StousleReraceo!

Ta
RETAS

Ameneozore

wisca- Tryjille Formation

Third Goal Hormon
2yoor reer

Rio Guasare Formation 400-1000 reer
Gueyule Group

Guayule Shale
(aay include some Colon Shele in top)

Z000r FEET

La Lune Formation soo? reer

Cogollo Formation
1200 Feer

Rio Negro Formation soot reer

Palmarito Series

ee (goo reer

Rio Cachirl Series
Campo Chico Formation
z000! reer

de! Oeste Formation

45008 Fer

Grande Formation

e500! reer

‘=:

Sierra de Perijé Series

rooorreer

Seles by
fspered an Rio Cachiré in the Sierra de Perijé, Venezvele

LEGEND

sk dip in degrees
@, locality of collection
WE fault
Fe ee

unconformity

fiver,
a

channe! blocked by grest
Heite boulder on one side
Devonian bulder on ofher

e/,
Z
te pitsiuvc cnics ©

EPOX,

Locality from which Deranian fossils

mere collected in /926

Cafe Grande Form

Caio del Oeste Form

Campo Chico Form

@
—---N® Compe Chico Form
tyneous at eg ea

ae)

@ GY Paimerita From
o)

<u ot COM>
& Znology
APR 13 1943

BRa¥

th CAMPO
S/S TALS BOCAS

Pe |
_ BULLETINS or AMERICAN PALEONTOLOGY , Vol. 27.N

Pach enimels can go ne farther west

PLAYA LA INDIA.

Mevotain front of the Sierra de Pari)

Lomer and Middle Eocene age

eh _- eae

0. 108, 1943

Rio CACHIRI SECTION AND StTaTrions.— Liddle, ro42

Pu. 27, VOu. 27 Buu. AMER. PALEONT. No. 108, Pu. 1

Fig. 1—Photo 9 of fossiliferous, gray, Middle and Lower Devonian shale
at the top of the Cano Grande formation on the Cafio Grande branch of
Rio Cachiri. The bluffs are vertical and 60 feet high.

OOS jena

Fig. 2—Photo 10 of calcareous, gray, fossiliferous shale which forms

vertical bluffs 75 feet high on the Cafio Grande branch of Rio Cachiri.

Stratigraphically this locality is 200 feet lower in the section than the
locality of Photo 9.

Pu. 28, VoL. 27 Buu. AMER. PALEONT. No. 108, Pu. 2

Fig. i= Ph eta 3 aie gray, slaty shale and gray Crodelan shale fat mamiets

brownish gray. Some dark-gray quartzitic sandstones are interbedded

with the shales. The locality is about at the top of the Cafio del Oeste
formation on the Cano Grande branch of Rio Cachiri.

£ ow a Pas efi: ¥* &
Fig. 2.—Photo. 7 of a massive bluff of thickly reddea aed black shale
containing a 30-foot layer of dense, black diorite. The locality is in the
lower part of the Cajio del Oeste formation on the Cafio Grande branch
of Rio Cachiri.

Buu. AMER. PALEONT. No. 108, Pr. 3

PL. 29, Vou. 27

‘TES O}f10rTp oy} weyy
WOT}OOS OY} UI IOYySIY op} eB ATTeoTydeisyeys 1aTyORD

JO 9 0J0YG—% “SLT

bata =

TITpOVN ONT FO yousrq epuely oUeO oY} TO
WOTPVMIOF 94SEQ [OP OUBD OY} FO O[PprmM oY} ynoqe st
YOTyM AFITBOOT STU} 7B SIND9O0 Opl[spUB] osIe, YW ‘ou0}SuOIT
-Aevlo JO sioXVT UY} suTezU0D yey} oeYys AVeIS ‘HORTG
Y}IM poppeqiezUr st 4J ‘omnjoerz Ar10jQvYys eB Suey

greys Avo “yovlq-ystkeis ‘Iepou jo F oJoYg—T ‘Siz

—

be Fen *

BPs} Rro Cacnirt Fossit,s : HARRIS 55

PART II, PALEONTOLOGY
A: BRACHIOPODA AND MOLLUSCA
By

G. D. Harvis

At the request of Mr. R. A. Liddle, I have prepared the follow-
ing brief statement relative to the collection of molluscs and
molluscoids, mainly Devonian, he has recently made in western
Venezuela.

Like the Cachiri River collection of Yeakel and Liddle, report-
ed upon by Weisbord (1926), and the Floresta fauna of Olsson
and Dickey, reported upon by Caster (1939), we have here a pre-
dominatingly brachiopod and bryozoan fauna with molluscs and
trilobites playing subordinate roles. We miss the usual South
American developments of fair-sized modiomorphids, nuculids,
Conularias, ef al., among the molluscs, as well as the most usual
austral brachiopod types—Spirifers with few broad ribs, Lepto-
ceelias, Orbiculoideas, and Rensellerias. Stropheodonta and
Chonetes are fairly abundant and, with them, representatives of
eltrypa reticularis, Athyris spiriferoides,

the far-ranging types
Tropidoleptus carimatus and Amphigenia elongata.

In this particular collection we have found no traces of trilo-
bites. This may be only accidental, however, since a few have
been found in the Floresta and Cachiri collections mentioned
above.

With the limited amount and imperfect state of preservation
of the material at hand, it would be rash to attempt delimiting
higher systematic units than species and subspecies at this time,
though novel and interesting features may well be pointed out and
illustrated. That these northwestern South American faunas are
rich in old and new types there can be no doubt, and a great
addition to the world’s Devonian history will be made as soon
as time and opportunity permit of making extensive collections,
coupled with detailed stratigraphic observations over wide areas.

The general aspect of the collection inclines us to regard it as
mainly representing approximately Onondaga time in North
American geologic chronology,

The frequent occurrence of meristellids and platycerids may
even suggest Oriskanian affinities at some localities. The absence

56 BULLETIN: 108 324

of representatives of the far-flung cuboidal and pugnax-like rhyn-
chonellids, Stringoce phalus, Buchiola and Grammuysia would seem
to preclude definite relationships between this and upper boreal
Devonian developments. The presence of rather large productids
in “float” material raises the question of the possible presence of
Carboniferous deposits about the Cachiri basin.

All specimens are deposited in the cabinets of the Paleontologi-
cal Research Institution, Ithaca, N. Y.

Noves ON BRACHIOPOD SPECIES
Genus RHIPIDOMELLA O’Ehlert, 1890
Jour. de Conch. 3d ser., vol. 38, p. 566
Genotype—Terebratula michelini Léveillé, Fischer, (1887, p. 1288).
Iustration.—Orthis (Rhipidomys) michelini Fischer, Man’! de Conch.,
1887, p. 1288, fig. 1057.

Rhipidomella liddlei, n .sp. Plate 4, figs: l-da

In the collection under consideration there are flat pedicle
valves of Rhipidomella (outside and inside surfaces) and a large,
very ventricose, brachial valve, all figured herewith. At first we
had supposed these might be referred to Orthis hartti of Rathbun
or perhaps to Orthis subcarinata (Hall) Knod. However, it ap-
pears from Rathbun’s description that hartti is far more nearly
equivalve than our species and has the ventral valve depressed
longitudinally in the center. Knod’s subcarinata shows a dorsal
depression, as does ours, but the form is more pointed umbonally.

So far as cardinal process and crura are concerned, this Vene-
zuelan species seems to be well represented by Hall and Clarkes’
figure of Rhipidomella penelope (1892, pl. 6A, fig. 10). There
is practically no cardinal area.

Locality.—Stations 64, 65, 72.

Genus DALMANELLA Hall and Clarke, 1892
Geol. Survey New York, Paleont. vol. 8, pt. Ep: 205

Genotype.—Orthis testudinaria Dalman, K. svenskn Vet.-Akad. Tanda.
SZ hwo Wl een tes te

[lustration.—Hall and Clarke, Geol. Survey New York, Paleont., vol.
8, 13925 (pt. Ly ple Sb, figs. 27539).

Dalmanella, sp. Plate 4, fig, 5

A small specimen, seemingly quite close to the Orthis nettoana

25 Rio CacnHini FossiLs; HARRIS a7

io)

ol Rathbun (1874) p27, ple 10, fies. 7, 13), is represented in
this collection from Sta. 65. Somewhat similar forms are repre-
sented by Knod (1908, pl. 26, figs. 9-11) as Orthis subcarinata
Hall, a common form from the “Shaly limestone” of New York.
Genus LEPTZENA Dalman, 1828
Genotype.—Conchita rhomboidalis, Wilekens, Nachr. von selten Verstein-
erungen, 1769, p. 77, pl. 8, figs. 43, 44—Schuchert
Iilustration.—Geol. Survey New York, Paleont., vol. 8, pt. 1, 1892, pl. 8,
figs. 17-31.
Leptwena rhomboidalis (Wilckens), sen. lat. Plate 4, fig. 4
That the material we have under consideration belongs to the
species rhomboidalis 11 a broad sense, there can be no doubt.
Specimens from the Floresta (Colombia) region are regarded by
Caster as constituting a distinct form, boyaca. See his discussion
of boyaca in volume 24 of these Bulletins, p. 119, 1930.
Locality.—Sta. 65.
Genus LEPTOSTROPHIA Hall and Clarke, 1892
Geol. Survey New York, Paleont., vol. 8, pt. 1, 1892, p. 288
Genotype.—Stropheodonta magnifica Hall, 10th Ann. Rept. New York
State Cab. Nat. Hist., 1857, p. 54; so designated by Hall and Clarke,
(1892, p. 288).
Ilustration—Hall, Geol. Survey New York, Paleont., vol. 3, 1859, pl.
93, fig. 4; pl. 94; fig. 2 a-d; Hall and Clarke, Geol. Survey New York,
Paleont.. voles, wt. UW W892* pie 13, fies: 27, 28)

Leptostrophia cf. concinna (Morris and Sharpe) Plate 4, fig. 6
Orthis concinna Morris and Sharpe, 1846, Quart. Jour. Geol. Soe. London,
vol. 2, p. 275, pl. 10, figs. 2 a, b.
Leptostrophia concinna Clarke, 1918, Mon. Serv. Geol. e Min. Brasil, vol.
Deez Scom ple or

The specimen we have figured as figure 6, Plate 4 seems to be
not far from Morris and Sharpe’s concinna, in fact resembling
the illustrations of that species more closely than it does the illus-
trations of New York Devonian members of this genus.

Locality.—Sta., 65.

Leptostrophia (Rhytistrophia) caribbeana Weisbord Plate 4, fig. 9

Leptostrophia caribbeana Weisbord, 1926, Bull. Amer. Paleont., vol. 11,
De 2oU ple oii, aio. Il.

Khytistrophia caribbeana Caster, 1939, Bull. Amer, Paleont., vol. 24, p.

18s.

In the material of this collection there is a large specimen un-
doubtedly of this species, but by no means so perfect as the spe-
cimens studied by Weisbord or Caster.

Locality.—Stations 65, 60.

a a9
58 BuLLETIN 108 526

Genus SCHELLWIENELLA Thomas, 1910
Mem. Geol. Survey Great Britain, Pal, 1, p. 92
Genotype.—Spirifer crenistria Phillips, 1856, originally so designated
by Thomas, p. 92.

Schellwienella goldringxe Caster Plate 4, figs. 7-8a
Sehuchertella aff. sulivani Weisbord, 1926, Bull. Amer. Paleont., vol. 11,

p. 232, pl. 37, fig. 2.

Schellwienella goldringw. Caster, 1939, Bull. Amer, Paleont., vol. 24, p.
216, pl. 13, figs. 1-3;

For a detailed account of this species, see Caster (1939) as re-
ferred to above.

Its general appearance is very much like that figured by
Rathbun (1874) for Hartt’s Streptorhynchus agassizi. It will be
noticed that the radii of figure 7 are much coarser and show more
distinct alternation in size than do those of figure 8.

Locality-—Sta. OI-J-113, and Sta. 65.

Genus DICTYOSTROPHIA Caster, 1939
Bull. Amer. Paleont., vol. 24, p. 160

Genotype.—Diclyostrophia cooperi Caster, Bull. Amer, Paleont., 19389,

vol. 24. 0. LUGO) ply 8; tess 72s ple LO} tiese9i lh, 2 eto ale

The data used in describing this genus were practically all de-
rived from the external and internal casts of one specimen from
the Floresta collection. We now have what appear to be speci-
mens of the ventral valve of this species and genus from the
Cachiri district,

Dictyostrophia cooperi Caster Plate 4, figs. 10-12
l‘or a very detailed description of the holotype (brachial valve),
see Caster as above referred to.

The details of the sculpture of the ventral (pedicle) valve vary
greatly in accordance with the layers exposed, as will be noted
from figures 10-12.

Locality.—Sta. 65.

Genus STROPHEODONTA®* Hall, 1852
Geol. Surv. N. Y., Paleontology, vol. 2

ae p. 65

Genotype.—Leptaena (Strophomena) demissa Conrad®**, So designated by
Hall (1852, p. 63).

Hall says he proposed the name Strophodonta in 1850; see Hall in
10th Ann, Rept. St. Cab. Nat. Hist., 1857, p. 138.

( onrad first described demissa under Strophomena and not Leptaena
as given by Hall.

327 Rio Cacuirt Foss1is: HARRIS 59

Iustration.—Slrophomena demissa Cou, Acad. Nat. Sei., Phila., Jv., first
ser., vol. 8, 1842, pl. 14, fig. 14, Hall and Clarke, Geol. Surv. N. Y.,
Pal., vol. 8, pt. 1, 1892, pl. 14, figs. 7-12; Willard, Penn. Geol. Surv.,
Jaymlille, (Er TW). GB Tok, alg, aes ale

Stropheodonta (Cymostrophia?) casteri, n. sp. Plater ties: lees

Among our material there is an interior cast of a large stropheo-
dontid. In some respects it would seem to belong to the assem-
hlage Caster (1939, p. 148, pl. 7, figs. 14-17) has styled Cymos-
frophia. But it is larger than species so referred, more sharply
geniculate and with muscular attachments very different from
those of C. schucherti Caster (1939, pl. 8, fig. 6). The flabellate
diductor impressions are widely separated anteriorly by anterior
diductor scars within which are deep, elongated radial pits; pos-
terior adductors are broadly expanded, and pits indicate a cardinal
process of unusual dimensions, The cast shows fine papille
radially distributed ; the interior of the shell was accordingly punc-
tate. A very limited area is so preserved as to show the exterior
had radial lines of two sizes—heavy, with from two to five lighter
ones between—and indicating the surface may have had the pe-
culiar dimpled markings so characteristic of Cymostrophia,
though this appearance may be due to lateral crushing.

The assignment of this form to a definite section of the stro-
pheodontids must await more material, especially of the brachial
valve.

Locality.—Sta. 14.

Genus STROPHONELLA Hall, 1879
28th Rept. N. Y. St. Mus. Nat. Hust., p:- 154

Genotype.—Strophomena semifasciata Hall, 1863, p. 210, designated by
Miller, N. A. Geol. and Pal., 1889, p. 383.

Ilustration.—Hall and Clarke, Geol. Surv., N. Y., Pal. vol. 8, [tome
1892, pl. 12) figs. 4, 5.

,

?Strophonella cf. meridionalis Caster Plate 5, figs. 3-5

2Strophonella meridionalis Caster, 1939, Bull. Amer. Paleont., vol. 24,

De OM ple LO fio~ 10:

We strongly suspect this large cast to be the brachial valve of
Caster’s S. meridionalis. Yet, with but one specimen to study,
final conclusions cannot be made. The markings on the cast are
well shown in figure 3, but the cardinal area seems most remark-

oo
bo
on

60 BULLETIN 1085

able. This is unusually wide and seemingly without stropheo-
dontid denticulation. The left half of the cardinal process is
shown at c (fig. 4) and the left crura at p, but the right repre-
sentatives of both are somewhat broken.

With only the material now in hand, we know of no genus to
which this form can certainly be assigned. Further suggestions,
however, will doubtless arise as new material is available for
study.

Locality.—Sta. 34. As the material from this station is desig-
nated as “float” its horizon is as vet undetermined.

Genus TROPIDOLEPTUS Hall, 1857
10th Ann. Rept. New York State Cab. Nat. Hist., p. 152

Genotype.—Strophomena carinata Courad, 3d Ann, Rept. New York State
Geol. Survey, 1839, p. 64; so designated by Hall (1857, p. 152, as
given above).

Ilustration.—Hall, Geol. Survey New York, Paleont., vol. 4, 1867, pl. 62.
Tropidoleptus carinatus (Conrad) Plate 5, fig. 6

We have an imperfect specimen of what appears to be a repre-
sentative of 7. carinatus (Conrad) as it has been interpreted in
South American paleontology. The Morgan Expedition of 1871
obtained several specimens of this tvpe from Ereré, and Rathbun
described them in considerable detail, figuring three specimens
(8745p. 254,-pl. 9; figs. 1, 9; pli 10, fic. 26). 7 Mater (yeleeas
1870, p. 34) he wrote: “The description of the Brazilian form,
in the Bulletin of the Buffalo Society of Natural Sciences, re-
ferred to above, was made from a few specimens collected at
Frere in 1871. The collection made by the Geological Commis-
sion in 1876, however, contains many varieties resembling more
closely the species as it is known in N. America. This last collec-
tion has also many very large specimens...” “Rare at the
Ereré locality. (Morgan Ex. 1871; Geol. Comm., 1876.) Very
abundant on the Rios Maecurti and Curud. (Geol.

Comm.,
1876).

This species was also found by Mr, A. Agassiz, associ-
ated with litulina pustulosa, in Devonian deposits on the island
of Coati, Lake Titicaca, Bolivia.”

Regarding Bolivian occurrences Ulrich remarks: “Die unter-
suchten Hxemplare wurden von Sttibel in einem Grauwacken-
sandsteine im Thale des Rio Sicasica zwischen La Paz und
Oruro gefunden, wo sie, in gleicher Vergesellschaftung wie auf

329 Rro Cacti Fossins: HARRIS 61

der Insel Coati, mit [iulina pustulosa Hall zusammen vor-
kommen.” (N. Jahr’b. Min., Geol. u. Paleont., B. B., vol. 8, 1893,
Di75s)

Katzer (Grundz. Geol. Unter. Amz. Geb., 1903, pl. 10, figs. 6,
7) shows forms from Ereré and the Maecurt resembling very
closely the North American carinatus and the European rhenanus ;
to the latter he gives the varietal name 7. carinatus var. maecur-
uensts (op. cit. p. 271).

Our specimen is by no means perfect enough to admit of re-
ferring to any special varietal form, but it does show that, like
Amphigenia elongata, Tropidoleptus carinatus, sensu lato, it is
represented in the Devonian fauna of Venezuela.

Genus CHONETES Fischer de Waldh., 1830-37
Oryct. du Gouv. de Moscou, pt. 2, p. 134
Genotype.—Chonetes sp.=C. variolata d’Orb., fide, De Koninck (1847,
p. 209).
Illustration.—De Koninck (1847, pl. 19, fig. 5, pl. 20, figs. 2 a-1).
Chonetes (Eodevonaria*) subhemispherica Weisbord
Plate 5, figs. 7-9; Plate 6, figs. 1-4
Chonetes subhemispherica Weisbord, 1926, Bull. Amer. Paleont., vol. 11,
JO eo, [Olly ail aitee, OE

Chonetes venezuelensis ? Weisbord, Ibid., p. 254, pl. 37, fig. 8.

Chonetes subhemispherica ? Weisbord, [bid., p. 234, pl. 37, fig. 10.

Hodevonaria imperialis var. parva Caster, 1939, Bull. Amer. Paleont.,

VOM 24 py 226. pl. Ws, hes) I, dG:

We have refigured Weisbord’s holotype for convenience 1n
reference here and, by referring to Hall’s figures (1867, pl. 20,
figs. 6a, b) of C. hemispherica, the appropriateness of the name
subhemispherica is readily appreciated. To what extent less in-
flated and more circular forms like C. venezuelensis and varie-
ties, as well as larger, more inflated, forms like imperialis, can
be referred to one and the same species depends on the amount
and character of material that will be found in the future. Rathbun
says in describing his C. freitasi from Rios Maecurt and Curua
(187g; p: 20))::

In this species we have included a number of forms, which might
have served for the formation of several species were not the material
in our possession so abundant as to afford a complete series of variations,
uniting the different forms closely together. The younger shells are pro-
portionately the narrower, and in after growth they increase more rapidly
in width than in length.

Kodevonaria, Breger, Amer, Jr. Sci., vol. 22, 1906, p. 534. Genotype
C. areuata Hall.

62 BuuLuetTiIn 108

ioe)
oO
foo)

Of the larger forms, this author states that the nearest New
York representative “seems to be C. acutiradiata Hall. “Wines
in turn, is not far from C. hemispherica Hall (1867, pl. 20, figs.
5.6). All of which seems to suggest caution in giving new spe-
cific names. while at the same time the desirability of publishing
as many figures as possible of the few and fragmentary speci-
mens found thus far.

Locality._—Sta. 05 and 69.

Chonetes (Eodevonaria) venezuclensis Weisbord Plate 6, figs. 5, 6

Choneles veneznelensis Weisbord, 1926, Bull. Amer. Paleont., vol. 11,

p: 284, pl. 37, figs. 4, 5, 87

One great difficulty in identifying the material in hand is that
specimens are generally more or less coated over with a film not
dissolvable in any ordinary acid solution. Such surfaces as are
Jaid bare seem to indicate that there is a species less inflated than
subhemispherica and with finer radii than characterize that spe-
cies. These are called venezuclensis by Weisbord and are re-
ferred to several variations of imperialis Caster by Caster (1939).

Locality.—Sta. 65.

Chonetes sttbeli Ulrich Plate 6, fig. 7

Chonetes stiibeli Ulrich, 1892, Neues Jahrb. Min, Geol. u. Paleont., Beil.-

Bde, vols S$) p. S0;splo o> figs: 3, 4:
Chonetes zulicnsis Weisbord, 1926, Bull. Amer. Paleont., vol. L1, p. 293,

Mle pale THON Ai.
Uie aff. billingsit Caster, 1939, Bull. Amer. Paleont., vol. 24, p. 232
De OS ee
Along with the larger, broader, chonetoid forms in the Liddle
collection, there are smaller, higher, fewer-ribbed representatives
that seem to be very close to Ulrich’s C. stitbeli and for the pres-
ent may well be referred to that species, though the broad fram-
ing of some of Rathbun’s lower Amazonian species may include
varieties comparable to these Venezuelian types. With the
material we now have in hand, positive specific assignments
seem quite out of the question.
As regards the occurrence of this species, Ulrich (1882, p. 81)
Says:
The species is found with Vituling pustulosa Wall, Tropidoleptus carin
utus Con, and Tentaculites sp. in shaly sandstone in the valley of Rio

Sicasica between Oruro and La Paz (Stiibel) possibly in the horizon of the
Huamampampa sandstone.

Rio Cacnirnt Fossius: HARRIS 65

Locality. Star 60.

*“Kodevonaria imperialis Caster” Plate 6, figs. 8, 9

Kodevonaria imperialis Caster, 1939, Bull. Amer. Paleont., vol. 24, p.

229 pl. 13, fig. 13.

The very large cast we have in hand is probably conspecific
with Caster’s imperialis though it is about 50 per cent larger than
his largest specimen (holotype). Hall and Clarke (1892, pl. 16,
figs. 35, 30) illustrate a specimen from the Corniferous limestone
near Williamsville, N. Y., which bears considerable resemblance
to this species, in which the identification of the adductor and
diductor muscular scars likewise seems uncertain.

Locality.—Sta. 69.

Genus CAMAROTCECHIA* Hall and Clark, 1894
Geol. Survey New York Paleont., vol. 8, pt. 2, p. 189
Genotype.—Atrypa congregata Conrad, 5th Ann. Rept. New York Geol.
Survey, 1841, p. 55, designated by Hall and Clarke, Geol. Surv. N. Y.,
Pal. vol. 8, 1894, p. 190.

Ilustration.—Hall, Geol. Survey New York, Paleont., vol. 4, 1867, pl.
D4, figs. 44-59.

Camarotechia, sp. Plate 6, fig. 17

An imperfect specimen from Sta. 65 seems to belong to the
rhynchonelloids of the Amazon region as described by Rathbun
(1879, p. 33) rather than to the centronellids as described from
Ponta Grossa by Clarke (1913, p. 211, pl. 22, figs. 1-7). We
have nothing comparable to the large “Rhynchonella’ ererensis
of Rathbun, but in his discussion the forms he refers to as
Rhynchonella (Stenocisma) dotis Hall (p. 33, of. cit.) seem to
tally fairly closely with the fragment in our collection. How-
ever, comparing it with Hall’s figures in volume 4 of the Paleon-
tology of New York, our specimen seems to conform most close-
ly with figures 21 and 22, Plate 54A named Rhynchonella (Sten-
ocisma) carica from the Hamilton stage of the Devonian from
Hamilton, N. Y. The fragmentary specimen figured by Caster
(1939 , pl. 13, fig. 21) from the Floresta fauna appears to be of
the species in hand. Katzer’s Camarotachia dotis (1903, pl. 10,
fig. 5) shows a specimen with 15 coste while ours had at least
twenty.

In ‘An Introduction to the Study of the Brachiopoda,’’ pt. 2, 1894,

p. 826, (13th Ann. Rept. State Geologist), this genus is given as ‘‘ Camaro-
toechia Hall, 1892,’’? without references.

64 BULLETIN 108 332

Genus DICTYLOCLOSTUS Muir-Wood, 1930
Annals and Mag. Nat. Hist. (10) vol. 5, p. 105

Genotype.-—Productus semireticulatus (Martin) Petrif. Derbiensia, 1809,
Dats Dison moss We 2 eile oa ndloe it.

[lustration.—See Martin, supra; Salter, Quart. Jour. Geol. Soc, London,
1861, vol. 17, pl. 4, fig. 1; Derby, Bull. Cornell Univ., Sci., No. 2,
1874, pl. 7, figs. 5-7, 15, 16; Hall and Clarke, Geol. Survey New York,
Paleont., voles; pti, 8925 pls WAR ness 16-18:

Dictyloclostus liddlei, n. sp. Plate 6, fig. 10

Although this specimen is imperfect in some details it appears
to belong to a form of productid with distinet radial ornamenta-
tion, with comparatively few spines. The latter, however, show
plainly on the ears exposed. The coste tend to show a tripartite
arrangement, most obvious where solution has taken place. <A
tendency toward this type of costation is shown in P. costata
Sow. de Noninck, (1847. pl She, 3b pl 18, te. 2) andl ees
scabriusculus (Martin) Whidborne (1897, pl. 20, fig 1.6). Pro-
ductella arctirostrata Hall (1867, pl. 26, figs. 22, 23) from the
Chemung Devonian of southern New York bears some resem-
blance to this species, but P. newberryt Hall (1892, pl. 18, fig. 3)
from the Waverly of Ohio makes a much closer approach.

Locality.—Sta. OI-J-113 “Float’’.

In general, the productids seem strangely rare in South Amer-
ican Devonian beds, though decidedly common in the Carbon-
erous. Rathbun described a single imperfect specimen of P.
maeccuruensis Kathbun (1878, p. 17), comparing it to Hall’s fig-
ure of P. navicella from the Corniferous limestone of New York.
One small specimen, Productella cf. spinulicosta, has heen figured
by Caster (1939, pl. 13, fig. 20) from the Floresta fauna of
Colombia.

The holotype of this species has been crushed in by pressure,
and solution has etched out in unnatural prominence the central
disc portion; vet its size and most obvious characteristics seem
to suggest affinities with forms considerably higher than the De-
vonian beds found in place on the Cachiri River.

Dictyloclostus ? sp. Plate 6, fig. 10a

Among the specimens recorded as “float,” Sta. 38, we find a
fair-sized productid with fine radiate markings cut by lamellose,
transverse lines of growth, and with indications of scattered
spines. The stze and length of the latter are indicated in figure

10a, near the hinge margin. There can be no certainty in assign-

Rio Caciirt FOsstys: IARRIS 65

ing this specimen to any particular group of productids, but it,
as well as the preceding species, indicates that there are other,
presumably higher, fossiliferous horizons in the Colombo-Vene-
zuelan district not vet found in place.
Productella ? sp. Plate 6, fig. 11
A small, imperfect specimen of a productid is represented in
this collection from Sta. 65. It is very probably of the same spe-
cies as that figured by Caster as Productella ef. spinulicosta Hall

(MOO pa 22) ple ten tial20))
Genus AMPHIGENIA Hall, 1867
Geol. Surv. New York, Paleont., vol. 4, p. 382

Genotype.—Pentamerus clongatus Vanuxem, 1842, Rept. 3d Dist. Geol.

Survey New York, p. 152, so designated by Hall, (1867, p. 382)

Illustration —Hall, op. cit., 1867, pl. 59, figs. 1-11.

Amphigenia elongata var. weisbordi, n. var. Plate 6, figs 12-16

Amphigenia clongata Rathbun, 1878, Boston Soc. Nat. Hist., Proe., vol.

20, p. 34.

Amphigenia ? sp. indent., Weisbord, 1926, Bull. Amer. Paleont., vol. 11,

pl. 38, fig. 1.

In Clarke’s “Author’s English Edition” of his Paleozoic
Faunas of Para, Brazil (1899, p. 89), he says:

The abundance of typical specimens of Amphigenia elongata in both
the Maecurt and Curua sandstones is one of the most striking characters
of these brachiopod faunas.

Rathbun notes that the Brazilian specimens are not radially
striate (op. cit., p. 35), but regards this as possibly due to coarse-
ness of embedding rock. He, as well as Hall (op. cit., p. 383),
notes the extreme variability in form of this species. Reoanaite
New York representatives, Hall says

This fossil is extremely variable in form; in the young state it is often
as wide as long or wider, the hinge line extended, and the greatest width
a little below the hinge, rapidly narrowing to the front. Other specimens
of similar age are broadly ovate or oval, the dorsal valve depressed-con-
vex, ete.

So far, in Venezuela, only the broad, Athyris-like forms have
been found.

With only the imperfect specimen shown by Weisbord (op.

pl. 38, fig. 1) its systematic position could only be guessed
at, and certainly Weisbord made a good guess, for we have re-
cently sectioned and polished the same in such a way as to make
its characters evident. The illustrations herewith given show
clearly the nature of the specimen. The surface of the shell is

<<

66 SULLETIN 108 Be

not sufficiently preserved to show distinctly whether radiating
striz are present or not. Weisbord (loc. cit.) believes he found
traces of such stria. On a very limited area there appear, when
examined under the microscope, to be elongate radial pustules.
The spondylium comes to a V-point at about one-half the depth
of the shell where the point rests on a medial septum. Both are
composed of exceedingly thin shell matter. The septum extends
to the anterior edge of the shell, but shows little indication of a
thickening posteriorly as indicated by Hall’s figure 11, plate 59
(Opmcie):

Among the specimens discussed in this report, there is but one
belonging to this genus, a brachial valve from Locality 65.

Though doubtless of the variety here discussed, it shows an
enormous thickening of the rather flat dorsal valve, rather char-
acteristic, we should suppose, of a fully mature form. Yet its
outline is broad athyrid. The foramen, as indicated by Hall in
his figure 7, plate 59 (op. cit.), is present, but the crural supports
are broad and separated by a wide sinus.

Doubtless detailed study of the North and South American
forms will bring out further distinctions, though whether of spe-
cific importance will depend on individual judgment. At any
rate, here seems to be an important and most characteristic
“Schoharie Grit” form, wide-spread and often abundant in nor-
thern South American Devonian beds.

Genus ATRYPA, Dalman, 1828
KK. Vetens. Acad. Hand, Stockholm, 1827, vol. 98, p. 102

Genotype.—Anomia reticularis Linn, 1767, Syst. Nat., ed. xii, p. 1152.
Atrypa reticularis var. harrisi Caster Plate 6, fig. 18

When we see these goodly-sized, expansive reticularid forms,
we note at once a close relationship with the type long ago styled
A. desquamata Sowerby (1840, pl. 56, figs. 19, 20). (See also
Davidson, Paleont. Soc. London, 1864, pt. 6, British Dev. Brach.,
p. 56, pls., 10, 11). Hall (1867, expl. pl, 52) figs. 7-16)" femanks
regarding large forms from the Corniferous limestone of Albany
and Schoharie counties :

The speeimens present many features in common with the A. desqua-
mata ot Sowerby, but the shells are more gibbous and the beaks less ele-
vated. The foramen and deltidial areas are not preserved in our species
except in the young individuals. It is probable that they will eventually
prove to be specifically distinet from the smaller forms referred to A,
reticularis.

1

Rio CacuiriFossii,s: HARRIS O67

That the-reticularid form before us is specifically identical
with that illustrated by Weisbord from the headwaters of the
Cachiri River, there can be no doubt. (See -ltrypa cf. reticularis
Weisb: Bull Amer. Paleont. voli 11,1926, p. 237; ply 38, figs, 2
3). In the same group, presumably belong the somewhat 1m-
perfect forms described by Caster from the Floresta district of
Colombia (1939, vol. 24, p. 240, pls. 13, 16). All specimens thus
far considered seem to be of the ventral valve only, which is not
markedly gibbous; and one very imperfect impression before us
of a brachial valve would suggest a similar conclusion regarding
its form, At any rate we have here desquamata-like representa-
tives of the reticularid stock rather indicative of an Onondaga
horizon of the north Atlantic realm. The only objections to as-
signing them a new name, /rarrisi, as Caster has done, is that we
still lack information regarding the deltidium of the pedicle valve,
while the brachial valve is practically unknown. Again, new
names at once obscure all relationships with well-known species.

I-or examples of the plasticity of this brachiopod type see the
Fenton’s article (1935, p. 309) “<ltrvpae described by Clement L.
Iebster and related forms (Devonian, Iowa)” and Stainbrook’s
(1938, p. 229) “Atrvpa and Stropheodonta from the Cedar Val-
ley beds of Lowa.”

Locahity.—Sta. 65.

Genus SPIRIFER Sowerby, 1815
Mineral Conchology, vol. 2, 1815, p. 41
Genotype.—dAnomites striatus Martin, Petr. Derb., 1809, pl. 23, figs. 1, 2;

so designated by suspension of Rules of Zo6l. Nom. (See Procedure
in Taxonomy, Schenk and MeMasters 1936, p. 55).
Illustration.—Spirifer striatus. See Martin, above; Hall and Whitfield
in King’s Geol. Expl. 40th Par., vol. 4, 1877, pl. 5, figs. 13-15.
Spirifer weisbordi, n. sp. Plate 6, fics: 19) 205) Plate. 7, fete
In the collection under consideration, there are two large spe-
cimens of Spirifer, badly eroded but showing general shape and,
locally, fine markings. One is figured herewith. Their most
striking character is the depth and breadth of the mesial sinus.
Ribs seem to be about 30 in number and are carried over the
sinus area as well as laterally. One is at once reminded of S.
divaricatus Hall from the Onondaga limestone of New York,
though the sinus of the latter species is a little more acutely de-
pressed centrally. The ribs are crossed by sharply marked con-
centric lines as in antarctica Morris and Sharp and kingi Caster,

6S 3ULLETIN 108 336

but the fine radiate markings sometimes shown in illustrations ot
these species are not preserved More specimens may show
closer relationship with kingi than now seems evident. Others
may indicate a relationship with the large cast referred to by
Caster (1939, p. 262, pl. 18, fig. 9) as Australospirifer cf. ant-
arcticus. Its size and bilobate appearance make this an outstand-
ing species in this fauna.
Locality.—Sta. 65)

Spirifer kingi Caster Plate 7, figs. 2-4
Spirifer kingi Caster, 1939, Bull. Amer. Paleont. vol. 24, p. 251, pl. 18,
figs. 1-4.

2Conocardium?, sp. indent. Weisbord, 1926, Bull, Amer. Paleont., vol. 11,
p. 246, pl. 40, figs. 4, 5.

A few casts of the interior of the pedicle valves indicate the
presence of Spirifers very closely allied to, if not identical spe-
ciheally with, king? Rib subdivision seems less general and the
“pustulate” appearance is less pronounced as the transverse
strize are less deeply incised than in the type specimen of kingt.
Not enough specimens of kingi or of these similar forms have
ever been collected to fully characterize them specifically. Hartt’s
pedroanus and ehize@e (Ikathbun, 1874, pl. 8, figs. 1-4) have similar
outlines, but lack the mesial costation of kingi, A very small,
young specimen is shown as figure 2 magnified about 6 times. An
adult is shown as figure 3, while the fine radial strize on the ribs
are shown by figure 4.

It seems quite possible that the broken and laterally crushed
specimen figured by Weisbord as Conocardium, vide supra may
be the remains of an adult specimen of this species.

Locality.—Stas. OI-J-97, 65:

Spirifer olssoni Caster Plate 7, fig. 5

Acrospirifer olssoni Caster, 1939, Bull. Amer, Paleout., vol. 24, p. 256,
pl. 18,: figs. 10-13.

Among the Spirifer fragments in the collection in hand, some
with few, strong coste are certainly different from kingi or the
Llytha groups illustrated by Caster. State of preservation does
not admit of differentiating such forms positively from the allied
antarctica or murchisoni, but they. are probably referable to
olssom Caster. Allan (1935, pl. 2, figs. 4, 5) has referred to a
somewhat similar form as “Acrospirifer cf. hystericus (Schlot. )”

Rio Cacnirt Fosstus: Harris 69

co
oo
~]

from the “Lower Devonian” of New Zealand. ‘The best speci-
men we have is crushed vertically as illustrated by figure 5, Plate
7, and if properly restored would he at least 50-- per cent wider
from beak to base.
Locality.—Sta. 63.
Genus ELYTHA Fredericks, 1924
Bull. Com. Géol. Petrograd, vol. 38, p. 304,—Neave
Genotype—Dellhyris fimbriata Con, Acad. Nat. Sei, Philadelphia, Jour.,
vol. 8, 1842,.p. 263.
Tustration.—Hall., Geol. Survey New York, Paleont., vol. 4, 1867, p.

214, pl. 33.
Elytha? plana, n. sp. Plate 7, fie. Ga

A much crushed specimen of this reticularid form 1s in the ma-
terial of the Liddle collection. Though wrinkled by pressure, there
are no signs of true radial ribbing, save the medial fold or plica-
tion. Almost microscopically fine radiating lines are present over
the shell surface, interrupted by concentric striae or lamelhe.
Such features recall those of Spirifer pseudo-lineatus Wall as
shown by Hall and Clarke (1894, pl. 36, fig. 29) from the Keokuk
limestone of Iowa. Having only an impression of the brachial
valve of this species, it is quite impossible to assign it to any genus
with certainty or satisfaction. Somewhat similar appearances
have been recorded among the athyrids, as one styled 4. royssii
L’Eveille by Walcott (1884, p. 280, pl. 18, figs. 9, 9a) in his paper
on the Eureka District and referred to the Lower Carboniferous.

The fineness and lengths of the segments of radial striation
seem to indicate that we have here quite a different type of orna-
mentation than that of the typical fimbriatus stock.

Locality.—Sta. 38, float material,

. Elytha colombiana Caster Plate 7, figs 7
Klytha colombiana Caster, 1939, Bull. Amer. Paleont., vol. 24, p. 246,
pl. 19, figs. 1-8.

2Delthyris fimbriatus Conrad, 1842, Acad. Nat. Sei., Philadelphia, Jour.
vol. 8, p. 263.

2Spirifer meridioamericanus Weisbord, 1926, Bull. Amer. Paleont., vol.
11, p. 238, pl. 38, figs. 4, 5.

Finer markings on the fragmentary specimens we have in hand
correspond well with the better material figured by Caster, but
the general shape of the shell is not shown. Turther collecting
will probably show the close relationship of all these forms and
the Onondaga expression of Conrad’s fimbriatus.

Locality.—Sta. 65.

70) BULLETIN 10S oar

Genus MERISTELLA Hall, 1860
13th Ann. Rept. N. York State Cab. Nat. Hist., 1860, pp. 74, 93
Genotype—Athyris levis Vanuxen, 1842; so designated by Hall and
Clarke, see N. Y. Geol. Surv., Pal. p. 76, vol. 8, 1894.
Illustration._-Hall, Geol. Survey, New York, Paleont., vol. 5, 1861, pl. 359.

Meristella wheeleri Caster Plate 7, fig. 8

Meristella wheelerit Caster, 1939, Bull. Amer. Paleont., vol. 24, p. 269,

pl. 18, figs. 14, 15.

The specimen figured by Caster, as well as that herewith
shown, indicates an unusually broad , deep medial sinus for mem-
bers of this genus. The preservation of the former is somewhat
hetter than in the latter, but that they may belong to one and the
same species there can be little doubt.

Localiy.—Sta. 69.

Meristella, sp. Plate 7, figs. 9, 9a

We herewith illustrate a specimen of what appears to be a
Meristella with no indication of a medial fold or sinus, hence
very different from wheeleri referred to above. In general ap-
pearance, this is intermediate between nasuta Conrad from the
Onondaga of New York and riskowski Ulrich from the “Icla-
schiefer” of the Devonian of Peru. With only this one specimen
in hand, it cannot be referred with assurance to Meristella, though
it probably has affinities with the meristids,

Though Meristella ranges from the Coeymans to the Tully lime-
stone in New York, it is most at home in beds not above the
(Onondaga limestone.

Locality.—Sta. 69.

Genus ATHYRIS M’Coy, 1844
Synop. Carb. Foss. Ireland, p. 146 (by Griffith)
Genotype.—Terebratula concentrica vou Bueh, fide Fisch, Man, Coneh.,
1887, p. 299.
[ustration.—Davidson, British Dev. Brach., 1864, pl. 35, figs. 11-18, pl.
4, figs. 1-3; Kayser’s Lehrb. Geol., Bd. 3, 1923, p. 249, fig. 6.

Athyris spiriferoides (Eaton) Plate 7, fig. 10
Terebratula spiriferoides BWaton, 1831, Amer, Jour. Sten Ol IL, joe, ILSY/
Athyris spiriferoides Hall, 1867, Geol. Survey New York, Paleont., vol.
4, p. 285, pl. 46.

Athyris aff. spiriferoides Weisbord, 1926, Bull, Amer. Paleont., vol. ae
p. 245, pl. 40, fig. 1 of the interior.

Though A. concentrica, a distantly related form, is character-

istic of the Upper Devonian of Europe (Davidson, 1864, p. 16:
: ie an a is wa : .

Hall, 1867, p. 288), A. spiriferoides is an Onondaga-Hamilton,

nid-Devoman species. Its occurrence in South America, first

noted by Weisbord, is quite in harmony with the wide range of

~l

339 Rro CacnirI Fossius: Harris

other virile stocks such as sltrypa reticularis, Amphigenia elong-
ata, Reticularia fimbriata, Tropidoleptus carinatus, etc. ‘To what
extent these South American representatives should receive spe-
cial names must await the results of more extensive investiga-
tions.
Locality.—Sta. 65.
Genus PENTAGONIA Cozzens, 1846
Ann. Lyceum Nat. Hist. New York, vol. 4, p. 158, pl. 10, fig. 3
CGenotype.—Alrypa unisuleata (— peersti Coz.) Conrad, 5th Ann. Rep.
Geol. Surv. N. Y., 1841, p. 56, so referred by monotypy.

Hlustration.—Meristella (Pentagonia) unisuleata Wall, Geol. Surv., N.
Y., vol. 4, 1867, p. 309, pl. 90, figs. 18-45.

Pentagonia? gemmisulcata Caster Plate 7, fies, 1, iia

Pentagonia gemmisuleata Caster, 1959, Bull. Amer. Paleont., vol. 24, p.

OT”

BH Jolle Wey, wiesy, AKG, Alec

For convenience in reference we have refigured Caster’s type
specimen but feel that more and better material is needed before
finally assigning it to Pentagonia or any other brachiopod genus.
May it not possibly belong to some unique aviculoid form. It is
really a unisuleate form as the illustrations show while the
gemmisuleate character applies only to the imprint (reversed)
specimen.
y As figure 13 we show another biplicate fragment from Sta.
65, vaguely suggesting a Myophoria-like form. Clarke (1909, p.
75, pl. 16, figs. 14, 15) has called attention to specimens from the
Moosehead Lake region of Maine (Oriskanian, Coblentzian)
closely resembling Prosocalus pes-anseris Beiler and \Virtgen,
a bicarinate [European dimyarian. ‘These fragments of unisul-
cate or bicarinate specimens, though scarcely now identifiable
specifically or even generically are so characteristically marked
that they will doubtless eventually serve a good purpose in paleon-
tologic stratigraphy.

~ PRLECYPOD SPECIES
Genus LIMOPTERA Hall, 1869
Prelim. Notice Lammellibranch Shells, ete., pt. 2, p. 15

Genotype.—Lima macroptera Con. Rept. New York State Geol. Survey
IS38, p. 117; original designation by Hall, 1869. p. 16.

j

[lustration.— Hall, Geol. Survey New York, Paleont., vol. 5, pt. 1, 1884,
pls. 24, 26-29,
Limoptera tenuis, n. sp Plate 8, fig. 1

The general erectness of the specimen herewith figured at once

72 BuLLETIN 108 34.0

suggests its relationship with the limopterids, though the thinness
of shell and the divaricate radii seem features scarcely in har-
mony with those usual to this genus. The large wing shows
clear-cut ‘concentric strize, while the body of the shell shows radi
varying in size and extent of bifurcation. The confusion in sculp-
ture above on the wing of the specimen figured seems due to the
impression of the ornamentation of the right valve through the
left valve.

We have seen no illustration of anything comparable to this
form from South America or elsewhere. Vague resemblances
may perhaps be found in comparing Hall’s L. pauperata (1884,
pl. 26, fig. 5) from the Onondaga of New York or Clarke sae
rosieri (1908, pl. 20, figs. 1, 2) from the St. Alban beds of New
Brunswick, but the height and remarkable tenuity of test seem
unique characters. A very indistinct impression, nearly smooth,
is found in material from Sta. 65, quite probably the internal im-
pression of this species; also an imperfect imprint of the exterior
of a left valve.

Locality.—Sta. 65/

Genus ACTINOPTERIA Hall, 1883

Geol. Survey New York, Paleont., vol. 5, pt. 1, 1884, p. 107
(Issued as Plates and Explanations only, Jan. 1883)
Genotype.—Actinopteria decussata Hall, designated by Bassler, U. 8.
Nat. Mars. Bulle Noy 92,1915; ip. 17.

[llustration—Hall, Geol. Survey New York, Paleont., vol. 5, pt. 1, 1884,
pl. 18, figs. 1-15.

Actinopteria subulrichi, n. sp. Plate 8, fig. 2

Among the specimens from Sta. 65, there is one referable to
the genus <Ictinopteria, as usually understood, having the general
form of decussata Hall and ulrichi Knod (1908, pl. 26, figs.
2), but without the sharply defined concentric lines of the former
and with very much finer radii than the latter. The radii vary
somewhat in size and occasionally show a tendency to alterna-
tion. The concentric striation is very faint.

This is not far from Whidborne’s hirundella from the Devon-
ian of southern England as figured in the Palaeontographical So-
ciety of London for 1892 (Whidborne’s monograph, vol. 2, pt.
2, pl. 6, figs. 5, 6). Comparison with Hall’s 4. subdecussata
(1st. Ann. Rept., State Geologist, for 1882, dated 1884) pl
Gg may likewise be made to advantage.

=;

aii:

541 Rio CACHIRI FossIus: HARRIS 73

Genus AVICULOPECTEN M’Coy, 1851
Ann. Mag. Nat. Hist., 2d ser. vol. 7, p. 171

Genotype.—A. planoradiatus M’Coy, so designated by Hind, Mon. Brit-
ish Carb. Lamell., vol. 2, 1903, p. 66.
Illustration.—St. Geol. Surv. Kan., vol. 10, 1957, pl. 5, figs. 12-15.

Aviculopecten yeakeli Weisbord 9 Plate 8, fig. 3

Aviculopecten: yeakeli Weisborid, 1926, Bull. Amer. Pal., vol. 11, pl. 5,
fig. 3, p. 244, pl. 40, fig. 3.

Fragments of specimens undoubtedly referable to ./!viculopec-
ten, sensu lato are found in the present collection and in the
Floresta material described by Caster, but so far, the most per-
fect specimen is the holotype of yveakeli here refigured for con-
venience in reference. Since this specimen is the imprint of the
interior of one valve the surface markings cannot now be well
defined. However, the early bifurcating of the ribs and the very
fine ribbing on the ear seem to be noteworthy specific character-
istics. or further details, see Weisbord, as referred to above.

Genus TELLINOMYA Hall, 1847

Geol. Survey New York, Paleont., vol. 1, 1847, p. 151
Genotype.

Tellinomya nasuta Hall, vide supra. The only species listed
by Hall under the primal generic diagnosis.
Ilustration.—Hall, Geol. Survey New York, Paleont., vol. 1, 1847, pl.
34, figs. 3 a-c.

Tellinomya ? sp. Plate 8, fig. 4

Owing to the apparent abundance of taxodonts indicated by
Clarke’s work on Brazil (1913, pl. 10), Méndez Alzola’s on
Uruguay (1939, pl. 10) and Ulrich’s on Bolivia (1892, pl. 2),
the Venezuelan fauna seems very poorly represented by this
type of Mollusca. The fragment herewith figured appears to
be the anterior end of a fairly large taxodont, showing very fine,
but sharp, concentric strize and unusually large taxodent teeth.
Its true generic affinities can only be determined when better
material is obtained. For similarly large dentition, see Whid-
borne (1896, pl. 7, fig. 10) Ctenodonta (Koenenia) cf. obsoleta
Goldf.

Locality.—Sta. 65.

Genus TELLINOPSIS Hall, 1869
Prelim. Note Lamm. Shells; St. Cab. Nat. Hist., 1869. p. 80
Genotype-—Nuculites subemarginata Con. (Acad. Nat. Sei. Phila. Jr.

Ist ser., vol. 8, 1842, p. 249, pl. 15, fig. 5) so designated by Hall, 1869,
p- SO). ;

Mlustration—See Conrad, supra, 1842, pl. 15, fig. 5; Hall, New York
Geol. Surv., vol. 5, Lamell. IT, 1885. p. 464, pl. 76, figs. 21-31.

74 BULLETIN 108 342

Tellinopsis? venezuelanus, 0. sp. Plate 8, fig. 5
Hall figures, on Pl. 70 referred to above, several more or less
elongated dimyarians with one or two ridges radiating out from
the umbo, especially posteriorly, and with posterior portion of
shell shorter than anterior, There is a somewhat Tellina-like ap-
pearance shown in some of these forms. Our shell is much
shorter proportionally with less well-defined umbonal ridge
and with a general Macoma-like appearance. On the shorter
moiety of the shell (which we are assuming to be the posterior )
the post-umbonal slope is rather narrow and shows signs of hav-
ing a faint radiating ridge near the shell margin. The surface of
the shell seems nearly smooth, though there are faint traces of
concentric lines. As a temporary expedient this shell is being
referred to Tellinopsis’? though with more and better material
a different generic assignment will doubtless be made.
Locaity-—Sta,Ole)|-113.) * Bloat.”

Genus EDMONDIA deKeninck, 1842

Desc. des Anim. fass. Carbon. Belg., 1842, p. 66.
Genotype.—Isocardia unioniformis Phillips (Geol. Yorkshire etc. 1836, vol.
2, p. 209, pl. 5, fig. 18); genotype, original designation by De Koninek,

p. 67.
[Hustration.—De Koninek (1842, pl. 1, fig. 4, a, b, ¢.), King, Perm. Foss.
ing., pl. 20, figs. 1-4; De Verneuil (1845, pl. 19, fig. 18).
Edmondia sylvana Hartt and Rathbun Plate 8, fig. 6
Edmondia sylvana Hartt and Rathbun, 1875, Ann. Lyceum Nat. Hist.,
New York City, vol. 11, p. 122.

Jdmondia sylvana Clarke, 1900, Paleosoie faunas of Parad, Brazil, Au-
thor’s English edition, p. 69, pl. 7, fig. 12.

Idmondia sylvana Katzer, 19038, Grundziige der Geologie des unteren
Amazonasgebietes, p. 206, pl. 14, fig. 12.

Since Hartt and Rathbun did not figure their Brazilian ma-
terial, there is some doubt as to the true character of this species,
but it seems probable that the small specimens we figure here-
with from Venezuela may belong to the same species figured by
Clarke and Katzer. However, the Amazonian specimens are
from two to four times as large as the specimens we have in hand ;
they are comparatively narrower and less produced anteriorly.

Locality.—Sta. 65.

wo
ns
o>

Rio CACHIRI Fossits: Harris 13)

Genus NUCULA Lamarck, 1799
Mem- Soc. No Hes Panis: pr 8/7

Genotype.—aArea nucleus Lin, Syst. Nat. 10th ech, p. 695, Nueula lam,
by monotypy.

Ilustration.—Grant and Gale, Mem. San Diego Soe. Nat. Hist., vol. 1,
1931, pl. 1, figs. 4, 5.

Nucula ?, sp. Plate 8, fig. 7

Clarke (1900, 1, pl. 8, figs. 9, 10) has illustrated a small Nucula
as “N. belhistriata Con., var. pervula, var. nov. from “Rio Mae-
cur” that bears considerable resemblance to our specimen. al-
though it is much larger. So far, we have not discovered any
trace of taxodont dendition in our specimen and hence it may not
be a Nuciula. It may be related to Cardiuiun greygarium Beaus-
chausen as illustrated by Clarke (1900, pl. 5, figs. 5-12) from
the Dalhousie beds of New Brunswick.

Locality.—Sta. OJ-J-113.

Leptodomus M’Coy, 1844
Leptodomus? ulrichi Clarke Plate 8, fig. 8
Leptodomus ulrichi Clarke, 1918, Foss. Dev. do Parana, p. 196, pl. 16,
figs? 195 20.

The only specimen in hand seems to be very close to that
shown by Clarke as fig. 20. Referring to the occurrence of his
specimens he states:

Associated with Leptocoelia and other characteristic brachio-
pods in the shales of Ponta Grossa; also, in the yellow shale of
Jaguariahyva; Sant’ Anna da Chapada and Lagoinha, Matto
Grosso.

Our specimen is likewise a vellowish, sandy shale, found lose
at Ol-J-113

With more perfect material in hand it will seem desirable to
assign this species to a new or more appropriate genus as the
name Leptodomus McCoy is preoccupied by Schoenhauer’s name
Leptodomus, 1843, according to Neave’s Nomenclator Zoologicus,
WO, 2:47), O11.

76 BuLLetTiIn 108 344

GASTROPOD SPECIES

Genus PLATYOSTOMA Conrad, 1842
Philadelphia Acad. Nat. Sci., Jour., Ist ser., vol. 8, p. 270
Genotype.—Platyostoma ventricosum Conrad, designated by Hall, 12th
Ann. Rept. Regents Univ. State of New York, 1859, p. 20.
IHustration.—Conrad, Philadelphia Acad. Nat. Seci., Jour., 1861, pu, Ike
fio. 5; Hall, Geol. Survey New York, Paleont., vol. 3, 1861, pl. 112,
figs. 1-10; Knight, Geol. Soe. Amer. Spee. Paper, No. 32, 1941, pl.
85, fig. 3a-d.

Platyostoma ventricosum Conrad Plate 8, figs. 9, 10
Platyostoma ventricosum Conrad, 1842, Philadelphia Acad. Nat. Sei.,

97

ANS, VOL: teh, joy Ma), jails Wife, aie,

Platyostoma ventricosum Hall, 1861, Geol. Survey New York, Paleont.,

vol; 3) p-. 469) ply War fies. IEi0:

Diaphorostoma ventricosum Clarke, 1908, New York State Mus. Mem.,

pt. 1p. 149, ple lo; tess Wi7-20%

The shell we are referring, temporarily at least, to the Con-
radian species ventricosum seems to agree generally with this
form, though perhaps showing a little more definite flattening
unmediately below the suture and lacking all trace of undulatory
ribbing. P. ventricosum is decidedly an Oriskany sandstone
species.

Locality.—Sta. 63, No. 6029.

Platyostoma ventricosum, var. permundum, n. var.
Plate: 8) figs: 115 12: Plate noasheas!

The specimen here so named is likewise from Station 63, and
its general characters are well shown by the three different views.
Its low spire and great mouth distinguish it at once from typical
ventricosum.,

Platyostoma neveritanum (Weisbord) Plate 9, fig. 2

Diaphorostoma neveritanum Weisbord, 1926, Bull. Amer,

Paleont., vol.
lip. 247, pl: 41.

By consulting Weisbord’s illustrations, it will be seen how very
naticoid the spire of the species appears, Our specimen is some-
what more depressed, but seems closely related to Weisbord’s.
The fine markings appear to be the same.

Locality.—Sta, 42.

Genus PLATYCERAS Conrad, 1840
Sd Ann. Rept. New York State Geol. Survey, p. 205
Genotype. Pileopsis vetusta Sowerby, designated by Tate (1870, p. 34).
Mustration—Knight (1941, pl. 88, figs. la-d), .

545 Rio Cacutri Fosstus: Harris 77

Platyceras sinistrum, n. sp. Plate 9, figs. 3, 3a
Owing to the fact that the characters of the: platycerids are
greatly modified by the objects they adhere to, specific differen-
tiation, as among the oysters, becomes a very difficult and uncer-
tain matter. The forms we have before us are without spines,
nodules or concentric undulations, and, upon the whole, seem
rather Helderbergian than Hamiltonian in affinities. The form
here styled sinistrwm is practically without surface ornamenta-
tion; the slight ridges seen in figure 2 are due to a flattening by
erosion. But there is a ridge shown by figure 3a marking off
what seems to be a wide umbilical area. The upward turning,
anastomate character of the aperture is an unusual feature.
Locality —Sta. 72. %,
Platyceras? gibraltar, n. sp. Plate 9, figs. 4-6
Since the apex of this rather large specimen is broken away
and the body of the shell lacks the more general irregularities of
Platyceras, considerable doubt is felt as to its systematic status.
The shell matter is much thicker posteriorly than anteriorly and
seems to have been perforated by numerous tubes as shown in
figure 6. The cast of the medial interior portion, as shown by
figure 5, is covered by fine, curved, radiating markings—perhaps
due to the work of parasites or marine organisms after the death
of the animal. The cast of the interior suggests that there were
larger, more or less Hipponya-like, radii on the exterior of the
shell. More perfect material must be obtained before this speci-
men can be properly classified.
Locality.— Sta. 42.

BIBLIOGRAPHY

Allan, R. S.
1935. The fauna of the Reefton beds (Devonian), New Zealand. New
Zealand, Dept. Sei. and Indust. Res., Geol. Survey Branch. Paleont.
Bull., No. 14, pp. 1-72, pl. 1-5, map.

Barrande, Joachim

1879. Systeme silurien du centre de la Bohéme, pt. 1, Recherches paléon-

tologique, vol. 5, Classes des Mollusques, Ordre des Brachiopodes, pls.
72-133.

BuLuETIn 108 546

~!
Go

Bassler, Kay ge '

1915. Bibliographical index of American Ordovician and Stlurian fos-
sils. U. S. Nat. Mus. Bull., No. 92, pp. 1-1521, 4 pls. (in 2 vols.).

Butts, Charles

1941. Geology of the Appalachian valley in Virginia, pt. 2, Fossil plates

und eaplanations. Virginia Geol. Survey, Bull., No, 52, pls. 64-155,
Caster, K. E.

1939. A Devonian fauna from Colombia, Bull. Amer, Paleont., vol. 24,

pp. 101-318, pls. 7-20.
Chao, Y. T.

1927. Productidw of China, pt. 1, Producti. Geol, Surv. China, Palwon-
tologia Sinica, Ser. B, vol. 5, Fascicle 2, pp. 194, pls. 16.

1928. Productide of China, pt. 2, Chonetina, Productine, Richthofinda,
Geol. Surv. China, Palwontologia Sinica, Ser. B. vol. 5, fase. 3., pp.
88, pl. 6.

Clarke, J. M.

1900 (1). The Paleozoic faunas of Para, Brazil, pt. 1, The Silurian fauna
of the Rio Trombetas, pt. 2, The Devonian Mollusca of the State of
Pard. Author’s English edition extraeted from the Archivos do
Museu Nacional do Rio de Janeiro, vol. 10, pp. 1-174, 1899 (‘‘ submit-
ted for publication, 1891’’), pp. 1-127, pls. 1-8.

1900 (2). The Oriskany fauna of Becraft Mountain, Columbia County,
N. ¥. New York State Mus., Mem., vol. 3, No. 3, pp. 1-128, pls. 1-9:

1908. Barly Devonie history of New York and eastern North Amertea.
New York State Mus., Mem., 9, pp. 1-366, pls. 1-48.

1909. Barly Devonie history of New York and castern North America.
New York State Mus., Mem. 9, pt. 2, pp. 1-250, pls. 1-34.

1913. Fosseis Devonianos do Parand. Serv. Geol. e Min. Brasil, Mon.,
vol. 1, pp. 12353, pls. 1-27.

Cleaves, A. B. See under Willard, Bradford
Cloud, Jr., P. E.

1942. Terebratuloid Brachiopoda of the Silurian and Devonian. Geol.

Soc. Amer., Spec. Papers, No. 38, pp. 1-182, pls. 1-26,
Conrad, T. A.

1838. Report of T. A. Conrad on the Palaecontological Department of the
Survey. State of New York, Assembly 200, Feb. 20, 1858, Commiuni-
cation from the Governor relative to the Geological Survey of the State,
pp. 107-119.

1840. Third annual report on the Palaecontological Department of the
Survey. New York-Geol. Surv., Ann. Rept., pp. 199-207.

1842. Observations on the Silurian and Devonian systems of the United
States with descriptions of new organic remains. Aead. Nat. Sei. Phil
adelphia, Jour., Ist ser., vol. 8, pp. 228-280, pls. 12-17.

1859. Observations on the genera Platyostoma and Strophostylus. 12th
Ann, Rept. Regents Univ. State of New York (Assembly Doc. No.
186) p. 20.

Davidson, Thomas

1864. 4 monograph of the British Devonian Brachiopoda, pt. 6 (1st see.).

Palwontog. Soc. (London), Mon., pp. 1-151, pls. 1-20.
Derby, O. A.

1874. On the Carboniferous Brachiopoda of Ttaituba, Rio Tapajos, Prov.

of Parad, Brazil. Bull. Cornell Univ., Sei., vol. 1.

No. 2, pp: 1-63. pls:
1-9. e :

547 Rro Cacuirt Fossmus: Harris 19

Fenton, C. L., and Fenton, M. A,

1935, Atrypae described by Clement L. Webster and related forms (De

vonian, Lowa). Journ. Pal. vol. 9, pp. 369-584, pls. 37-43.
Fischer, Paul
1880-87. Manuel de conchyliologic et de paléontologic conchyliologique,
pp. 1-1369, pls. 1-23.
Eaton, Amos
1831. Amer. Jr: Sci., Ist ser., vol. 21, p. 137.
Hall, James

1857. Appendia C. Descriplion of Paleozoic fossils. New York State
Cab. Nat. Hist., Ann. Rept,. No. 10, pp. 39-185, many text figs.

1859. Descriptions and figures of the organic remains of the Lower Hel-
derberg group and the Oriskany sandstone, 1855-1859. Geol. Survey
New York State, Paleont., vol. 3, pt. J, Text, pp. 1-532:

1861. Part 2 (of the above), pls. 1-120.

1867. Description and figures of the fossil Brachiopoda of the Upper
Helderberg, Portage and Chemung groups, 1862-1866. Geol. Survey
New York State, Paleont., vol. 4, pt. 1, pp. 1-428, pls. 1-63.

1869. Preliminary notice of the Lamellibranchiate shells of the Upper
Helderberg, Hamilton and Chemung groups, with others from the
Waverly sandstones, pt. 2, pp. 1-97, pages 1-80, primarily printed
edition of 100 copies, distributed in 1869, fide Hall: pp. 81-97, 1870.
(For a discussion of these dates, see Preliminary notice of the lamel-
libranchiate shells of the Upper Helderberg, Hamilton and Chemung
groups, pt. 1. 35th Ann. Rept. N. Y. St. Mus. Nat. Hist. by the Re-
gents of the Univ. of the State of N. Y., 1884, pp. 215-216.)

1879. The fauna of the Niagara group in Central Indiana. New York
State Mus. Nat. Hist., Ann. Rept., No. 28, pp. 99-210. pls: 3-37.

1884. Descriptions and figures of the Monomyaria of the Upper Helder-
berg, Hamilton and Chemung groups. Geol. Survey New York State,
Paleont., vol. 5 Dita eT) pps 1268: pls. 1-33, 81-92.

1885. Dimyaria (of the above), pt. 1 (2), pp. 269-561, pls. 34-80, 93-96.

Hall, James and Clarke, J. M.

1892. An introduction to the study of the genera of Paleozoic Braehio-
poda. Geol. Survey New York State, Paleont., vol. 8, pt. 1 pp. 1-367;
pls. 1-20.

1894. Part 2 (of the above), pp. 1-394, pls. 21-84.

Hind, Wheelton

1903. Monograph of British Carboniferous Lamellibranchiata. Palweont.

Soc. (London) Mon., vol. 2, 216 pp., 25 pls.
Katzer, Friedrich

1903. Grundziige der Geologie des untern A mazonasgebietes (des Staates

Para in Brazilien). pp. 1-296, pls. 1-16, map.
Kayser, Emanuel

1897. Beitrdge zur Kenntniss ein iger paldozoischer Faunen Siid-A mericas.
Zeits. der deut. geol. Gesel, bd. 49, pp. 274-317, pls. 7-12.

1878. Atlas von 36 lithographischen Tafeln zur Abhandlung iiber* dive
Fauna der éiltisten Devon-Ablagerungen des Harzes. Atlas zu den
Abhandhingen zur geologischen Specialkarte von Preussen und den
Thiiringischen Staaten, pls. 1-36.

Keyes, C. R.

1894. Paleontology of Missouri, pt. 2. Missouri Geol, Survey, vol. 5, pp.

1-266, pls. 33-56.

50 BULLETIN 108 348

King, Wm.

1850, Monograph of the Permian fossils of England. Paleontographical

Society. London, 4 to. pp. 1-258, pls. 1-28.
Knight, J. B.

1941, Paleozoic gastropod genolypes. Geol. Soe. Amer., Spec. Papers,

Nos 325 pp. L-oll0). plsid-96:
Keyserling, see De Verneuil
Knod, Reinhold

1908. Devonische Faunen Boliviens. Neues Jahrb. Min. Geol. u. Paleont.,

Beil.-Bd. 25, pp. 498-600, pls. 1-31.
Koninck, L. de

1842-1844. Description des animaux fossiles que se trouvent dans le
terrain carboniferé de Belgique 4+ to. Text pp. 1-716, pls. A-H and
ED

1847. Monographie des genres Productus et Chonetes. Recherches sur
les animaux fossiles, pt. 1, pp. 1-246, pls. 1-20.

Lambert, R. and Méndez-Alzola, Rudolfo

1958. Un nuevo yacimiento fosilifero devonico en el Departmaento do

Duwrazno. Inst. Geol. Uruguay, Bol., No. 24, pp. 169-174, pls. 3-15.
Liddle, R. A.

1928. The ueology of Venezuela and Trinidad. Ft. Worth, Tex. Royal 8

vO., pp. 1-552, pls. 1-83.
M’Coy, Frederick

S44. Synopsis of Carboniferous fossils of Ireland, 4 to, Dublin,

1846. Synopsis of the Silurian fossils of Ireland, 4to, Dublin,

1851. The British Paleozoic fossils added by Professor Sedgivich to the
Woodwardian Museum, 4t0, London.

(M’Coys 4 to. works not seen.)

IS51. Description of some new Mountain limestone fossils, Aun. and

Malice. Nat. Hist., 21 sér., vol. 7, pp. 167-175.
Martin, W.

1809, Pelrificata Derbiensia, or figures and descriptions of pelrifactions

collected in: Derbyshire, 52. pls.
Méndez-Alzola Rudolfo

1938. Fosiles Devonicos del Uruguay. Inst. Geol. Uruguay, Bol, No. 24,

pp. 1-115.
Miller, S. A.

1889. North American geology and paleontology. Roy. Svo. GGA, pp. 1194

text figs., Cincinnati.
Morris, J., and Sharpe, D.

S46. Description of eight species of brachiopodous shells from the
Paleozoic rocks of the Falkland Islands. Geol. Soc. Loudon, Quart.
Jour, vol. 2, pp. 274-278) pls. 10, 11.

Muir-Wood, Helen

1930. The classification of the British Carboniferous brachiopod sub
family Productine, Ann, and Mag. Nat. Tist., 10th ser. vol. 5, pp.
100-108,

Murchison, R. 1., see De Verneuil

349 Rio Cacitirt Fosstus: HARRIS 81

Neave, Sheffield Airey

1939-1940. Nomenclator Zoologicus, A list of the names of genera and
subgenera in zoology from the tenth edition of Linneus, 1758 to the
end of 19385. Svo, 4+ vols. London.

Nettelroth, Henry

ISS9. Hentuchky fossil shells—a monograph of the fossil shells of the
Silurian and Devonian rocks of Weuluchy. Wentucky Geol, Survey, pp.
-243, pls. 1-36.

Newell, N. D.

1937. Late Paleozoic Pelecypods: Pcclinacea, Kansas State Geol, Sur-

vey, vol. 10) pp. 1-125, pls. 1-20.
Phillips, John

1829. Illustrations of the geology of Yorkshire, or a deseripltion of the
strata and organic remains of the Yorkshire coast. 4t0, 15 pls. map,
York (2d ed., London, 1836).

1836. Part 2 (of the above). Zhe Mountain limestone district. 24. pls.
London.

S41. Figures and descriptions of the Paleozoic fossils of Cornwall, De-
von and West Somerset, observed in the Ordinance Geological Survey
of the district, Svo, 231 pp., 60 pls., London,

(Phillips articles, not seen)

Ochlert, D. P.

1S90, Note sur différents groupes Clablis dans le genre Orthis et en
particulier sur Rhipidomella Oehlert (Rhipidomys Ochlert, olim). Jour,
de Conch., vol. 38, pp. 366-374., fig.

Reed, F. R. C.

1903. Brachiopoda from the Bokheveld beds. S. African Mus., Ann.,
vol. 4, pp. 165-200, pls. 20-23.

1904. Mollusca from the Bokkeveld beds. 8. African Mus., Ann.,, vol. 4,
pp. 239-274, pls. 30-32.

1908. New fossils from the Bokhkeveld beds. S. Afviean Mus., Ann., vol.
4, pp. 381-406, pls. 47-48.

Salter, Js Ww.

1861. On the fossils from the High Andes, collected by David Forbes.

Geol. Soc. London, Quart. Jour., vol. 17, pp. 62-73, pl. 4.
Schuchert, Charles

1897. A synopsis of American fossil Brachiopoda, including bibliography

and synonymy. U.S. Geol. Survey, Bull., No. 87, pp. 1-464.
Schuchert, Ch. and LeVene, Clara M.
1929. Brachiopoda, (Generum et Genotyporum index et Bibliographica)
Fossilium Catalogus I: Animalia, Pars 42, pp. 1-140.
Sowerby, J. D. C.
1829. The mineral conchology of Great Britain. vol. 6.
Stainbrook, Merrill A.

1938. Alrypa and Stropheodonta from the Cedar Valley beds of Towa.

Jiour. Pal., vol. 12, pp. 229-256, pls. 30-35. :
Stoliczka, Ferd.

1871. The Pelecypoda, with a review of all known genera of this class,
fossil and recent. Paleontologia Indiea, Cret. Fauna 8. India, vol.
3, pp. 1-537, pls. 1-50.

Swartz, F. M., see under Willard, Bradford

82 3ULLETIN 108 350

Tate, Ralph
1870. Appendia to the Manual of Mollusca by S. P. Woodward. 85 pp.,
no plates.
Thomas, Ivor
1905. Nene Beitrige zur NKenntnis der devonischen Pawna Argeutinicis.
Deutsche Geol. Gesell., Zeitsehr., Ba. 57, pp. 283-290, pls. 11-14.
1910. The British Carboniferous Orthotetinw. Geol, Survey Great Britain,
Paleont., Mem., vol. 1, pt. 2, pp. 83-134, pls. 13.
Ulrich, Arnold
1892. Paleozoische Versteinerungen aus Bolivien. Neues Jahrb. Min. Geol.
u. Paleont., Beil.-Bd. 8, pp. 1-116, pls. 1-5.
Verneuil, Edouard de
1845. Geologie de la Russie d’hurope et des montagnes de lOural, par
Roderick Impy Murehison, Edouard de Verneuil and le comte Alex-
ndrie de Keyserling, 2 vols., vol. 2, Paleontologic, pp. 1-512, pls. 1-45,
and A-G.
Walcott, C. D.
1884. Paleontology of the Mureka District. U.S. Geol. Survey, Mon., vol.
8, pp. 1-298, pls. 1-24.

<
PLATES
PEA A C20)

Expenditure for engraving illustrations met by—

R. A. Liddle: 2 maps, 5 plates geologic views
G. D. Harris; 7 plates invertebrate fossils

BULLETIN 108

EXPLANATION OF PLATE 4 (30)

gure

Ihe

-]

10.

11,12.

Rhipidomella liddilei, n. sp.

Holotype, pediele valve: height 23, breadth 26, deptly 2

9)

m.: exterior of valve, somewhat eroded, Station 72, Pal.

Res. Inst. No. 5977.

Rhipidomella liddlei, n. sp.
Pediele valve, interior: height 20, breadth,
mim.: Station 65, Pal. Res. Inst., No. 5978,

Rhipidomella liddlei, n. sp.

Brachial valve: height, 30, breadth, 40, depth,

Station 54: Pal. Res. Inst., No. 5979.
Umbonal portion of fig. 8 enlarged. No. 5950.
Leptzna rhomboidalis (Wilckens)

Pedicle valve: height, 20; width, 28; depth,

tion 65; Pal. Res. Inst., No. 5981.
Dalmanella cf. nettoana Rathbun

Pediele valve: height, 7; width,

tion 65) Ral ines, Inst.) Noy ogs2:

7

Sige COTO UI

Leptostrophia conecinna (Morris and Sharpe)
Pedicle valve; height, 20; width, 22; depth,
tion 65: Pall Res. Inst.; No. 5983.

Schellwienella goldringz Caster

Bay

”)

dept ny

10

Winn. §

min. §

»)

Tithh. 5

Pedicle valve: height, 18; width, 26 mm.; Station OL-J-113,

‘‘Mloat’’. Pal. Res. Inst., No. 5984.

Schellwienella goldringz Caster

Pediele valve: height, 27; width, 38 mm.; larger specimen
showing traces of a thin median sepium and concentrie un-

dulations: Station OI-J-113' *‘ Ploat’’.: Pal: Res. Inst., No.

59OSD5.

Schellwienella goldringz Caster

Rubber cast of umbonal region of a small pedicle valve:

height, 13; width, 17 mm.; Station 65; Pal. Res. Imst., No.

D986.

Leptostrophia caribbeana Weisbord

Pedicle valve: height, 40; breadth, GO mm.; Station 69;

Pal. Res. Inst., No. 5987.

Dictyostrophia cooperi Caster

Pedicle valve: height, 85; width, 60; depth, 10 mm.; Sta-

tion 65; Pal. Res. Inst., No. 5988.

Maenified portions of fig. 10

Mn ly 2 s ‘ 0 .
Paken on geniculate area about half way from anterior to

right hinge terminal showing marked difference of

ornamentation at various depths from exterior.

Dictyostrophia cooperi Caster

Mragment of an inner layer of this species: Pal. Res. Inst.,

No. 5989,

shell

58

Pu. 30, Vou. 27 Buu. AMER. PALEONT. No. 108, Pu. 4

‘
Le
i
n
i
1
j
1
+
y
{
‘\

*
¥
’
1
ie
iy
rota
iy leach

Cam

irs

PLATE 5 (31)

,

86 BULLETIN 10S 354

EXPLANATION OF PLATE 5 (31)

Figure Page

1. Stropheodonta (Cymatostrophia?) casteri, n. sp. 59
Pedicle valve, cast: height, 50; width, 70; depth, 10) mm.;
showing general form of the holotype; from Sta, 64. Pal, Res.
Inst., No. 5990.

2. Same specimen as above, posterior area showing: a, remnants
of original shell; b, interior striations of shell; c, molds made
by cardinal processes of brachial valve; d, posterior adductor
sears; e, flabellate diductor scars; f, anterior adductor scars;
casts of radiate cavities.

2a. Punctate structure, anterior of fig. 1.

2b. Markings from left portion of fig. 1, cymostrophid?

3. Strophonella? cf. meridionalis (Caster) ~~ Sg
Cast of interior of brachial valve: height, 40; width, 55;
depth, 7 mm.; from Sta. 34. Pal. Res. Inst., No. 5991.

4. Cast of cardinal area of fig. 3; perfect crura and cardinal pro-
cess on left; those on right somewhat broken.

5. Details of central posterior portion of fig. 3.

6. Tropidoleptus carinatus (Conrad) eemee! Pemereres 3 =~ 160

Internal cast of brachial valve: height, 16; width, 20; depth,
1 mm.; from Sta. 65. Pal. Res. Inst., No. 5992.

. Chonetes (Eodevonaria) subhemispherica Weisbord —_ =a 61
Weisbord’s type specimen as figured in Bull, Amer. Pal., vol.
ILS Ao Olle aif, sales Ye

8. Chonetes (Eodevonaria) subhemispherica Weisbord
Pedicle valve: laterally compressed, and radii generally ob-
scured by a thick coating; height, 16; width, 12; depth, 9
mm.; from Sta. 65. Pal. Res. Inst., No. 5993.

9. Vertically compressed specimen of subhemispherica: height 14
breadth, 20; depth, 5 mm.; Internal cast of valve; surface
finely and highly papillate; from Sta. 69. Pal. Res. Inst., No.
5994.

4

PL. 31, Vou. 27 BULL. AMER. PALEONT. No. 108, Pu. 5

SEs es
she

ere

St
ia

PLATE 6 (32)

Inst., No. 6006.

12. Amphigenia elongata, var. weisbordi, n. var. 65
Pedicle valve: height, 25; width, 35; depth, 12 mm. The spe-
cimen figured by Weisbord (Bull. Amer. Pal, vol; 11) pl. 38;
ines, AL),

13. The same specimen, showing one limb of spondylium intact,
one broken.

14. The same showing median septum to the left, limb of spondyl-
ium to the right.

15. The same species: height, 35; breadth, 42; depth, 10 mm. Ex-
terior of brachial valve; Station 65. Pal. Res. Inst., No.
6007.

16. The same specimen as fig. 15.

Interior showing cardinal area where shell is very thick (but
very thin anteriorly) ; anterior margin badly broken, when in-
tact should be evenly rounded, not pointed as figured.

17. Camaroteechia sp. - ; 63
Height, 16; width, 16; depth, 3 mm. A specimen closely re-
sembling carica Hall from the Middle Devonian of New York.
Station 65. Pal. Res. Inst., No. 6008.

18. Atrypa reticularis, var. harrisi Caster . 66
Pedicle valve: height, 35; width, 34; depth, 4 mm; specimen
is broader than appears from the figure herewith given;
close to A. desquamata Sow. of the Devonian of England.
Station 65. Pal. Res. Inst., No. 6009.

19. Spirifer weisbordi, n. sp. : 6
Pedicle valve, cardinal view: height, 35; width, 55; depth,

15 mm. See also Plate 4. Station 63. Pal. Res. Inst., No.
6010.

20. The same species; slightly magnified; anterior medial margin,
showing type of costation; Station 68. Pal. Res. Inst., No,
6011.

~4

SS BULLETIN 108 356

EXPLANATION OF PLATE 6 (32)

: : IQ0'e
Migure Pag
1. Chonetes (Eodevonaria) subhemispherica Weisbord 6

Pedicle valve: height, 12; width, 16; depth, 4+ mm. ; show-
decoricated coarse ribbing; general contour and traces of
museular attachment; Station 65. Pal. Res. Inst., No. 5995.

bo

The same species, brachial valve; showing radiate folds and
muscular imprint of casts most commonly observed: height,
11; width, 20; depth, 3 mim. ; Station No. 65. Pal. Res. Inst.,
No. 5996.

3. The same species; cast of interior of pedicle valve more deep-
ly decorticated than shown in fig. 1, and showing muscular
attachments more clearly. Station No, 65. Pal. Res. Inst.,
No. 5997.

{. Presumably the same species, young, pedicle valve: height,
7; width, 10 mm. Sta. 65. Pal. Res. Inst., No. 5998.

5. Chonetes venezuelensis Weisbord 62
Imprint of exterior of brachial valve: height, 11; width, 15;
depth, 2 mm. Station 65. Pal. Res. Inst., No. 5999.

6. The same species, showing exterior of brachial valve above
and interior of pedicle valve below: height, 11; width, 14;
depth, 4 mm. Station 65. Pal. Res. Inst., No. 6000.

Ga, Chonetes venezuelensis? Weisbord
Pedicle valve, interior: height, 5; width, 10; depth, 1 mm.
Closely resembling some of the specimens figured by Clarke
as C. falklandensis (Mor. & Sh.) and C. Arcei Ulrich from
the Punta Grossa shales of southern Brazil. Station 358
“Wont. Pal. Res. Imst-.; No. 6001:

Chonetes stiibeli Ulrich BEET at i _ 6:
Pediele valve, cast of interior: height, 6; width, 7; depth,
2mm. Station 69. Pal. Res. Inst., No. 6002.

8. “Eodevonaria imperialis? Caster” Boeke eer el ts as WE EGS

Internal cast of pedicle valve: height, 25; width, 30; depth,

10 mm. Station 69. Pal. Res. Inst., No. 6003.

~]

9. The same specimen, cardinal view, showing arrangement of
muscular sears.

10. Dietyloclostus liddlei, n. sp.

St Se ee nee 64
Pedicle valve: height, 30; width, 30; depth, 10-+- mm. Main
portion flattened by pressure; ribs with tripartite markings;
Spine bases on ears only. Station OI-J-113, ‘‘Float’’. Pal.
Res. Inst., No. 6004.

10a. Dictyloclostus?, sp. = say ae ’ 64
Pedicle valve, interior cast: height, 15; width, 15; depth,

5 mm. Specimen crushed in sub-centrally; spine bases not
well shown. Station 38, ‘‘Float’’. Pal.. Res. Inst., No. 6005.
11. Productella?, sp. 65

arate Siler 0 aah aa "7 ; ;
Pedicle valve: height, 9; width, 9; depth, 2 mm. Compare

fig. 19, pl. 13, vol. 24, Bull. Amer. Pal. Station 65. Pal. Res.
Continued on previous page

Buu. AMER. PALEONT. No. 108, Pu. 6

PL. 32, VoL. 27

90)

BULLETIN 108 308

EXPLANATION OF PLATE 7 (33)

igure Page

1. Spirifer weisbordi, n. sp. at poe Se ee 67
Holotype; same specimen as figured « on a pl. 3, fig. 19.

2. Spirifer kingi Caster - SN 68
Pedicle valve, X5; from a rubber east, showing early type of
costation. Station OI-J-97 ‘‘Float’’. Pal. Res. Inst., .No-
6012.

3. The same species, nearly adult form: height, 18; width, 30;

depth, 5 mm. Station OI-J-97 “Float”. Pal. Res. Inst., No.
6012.

4. Portion of fig. 3 magnified to show fine radial striation.

5. Spirifer olssoni Caster be A a A Bt ee ee ee 68
Pedicle valve, vertically crushed, true height at least NGI
width, 30 mm. Station 63. Pal. Res. Inst., No. 6015.

6. Elytha? plana, n. sp. ies ee Ue Be ae 69
Holotype: brachial valve, rubber cast of exterior ; “height, 16;
width, 23; depth, 6 mm. Station 38. Pal. Res. Inst., No. 6014,

6a. The same; portion of surface enlarged.

7. Elytha colombiana Caster —— Ar ee (sk)
Brachial valve; height, 20 mm, Station 65. Pal. Res. Inst.,
No. 6015.

8. Meristella wheeleri Caster —_ pee ee Ul)
Pedicle valve, cast of interior, somewhat worn; height, 30;
width, 35 mm. Station 69. Pal. Res. Inst., No. 6016.

9. Meristella sp. BA oe a Se ee 70
Pedicle valve original shell matter, lexterion: height, 27;
width, 28; depth, 9 mm. Station 69. Pal. Res. Inst., No. 6017.

Ya. The same, interior showing umbonal characters.

10. Athyris spiriferoides (Eaton) ae a en 70
Pedicle valve: height, 30; width, 30; depth, 7 mm. Station
65. Pal. ‘Res: Imst., No Gols:

Ls Rentaconia? cemmisuleata Caster. 2222 = eee
Rubber cast from type specimen (See Bull. Amer. Pal., vol.

24, pl. 16, figs. 16, 17), vicinity of Floresta, Colombia,

[2,a. Pentagonia unisuleata Hall — ies SAL
After Hall. Here figured to show appearance of type ‘of the
genus,

13. An unidentified, myophora-shaped, somewhat eroded, specimen

showing remarkable bi-plication as in figs. 11 and 12, but
having more the appearance of a lamellibranch than of a
brachiopod: height, 20; width, 16; depth, 4 mm. Station
65.. Pal. Res. Inst., No. 6019 : = wooo loess

Buu. AMER. PALEONT. No. 108, Pu. 7

PL. 33, Vou. 27

92 BULLETIN 108 360

5

EXPLANATION OF PLATE 8 (34)

Figure Page
iy Limoptenal tenwis,ene espa. ee ee {fal
llolotype; left valve; height, 65; width, 45 mm.; Sta. 69;
Pal. Res. Inst., No. 6021.

2. Actinopteria subulrichi, n. sp. —-— Renee Te
Holotype; left valve; height, 23; width, 35; depth about 4
min. Wing evidently longer than shown, Sta. 65; Pal. Res.
Inst., No. 6022.

3. Aviculopecten yeakeli Weisbord —=.....____ ee

1. Tellinomya, sp. BI I ls ee ee 73

Anterior portion of right valve: height, 11; width, 18 mm.; «
Sta. 65: Pal. Res. Inst., No. 6024.

5. Tellinopsis? venezuelanus, n. sp. ~~. Der Sera ee teeter 28 See
Holotype; right valve: height, 18; width, 21; depth from 2

EO! Dl MIN Stas Olde Oat] ws allesinesenslonS hme Os
6025.
6. Edmondia sylvana Hartt — : ee

Right valve; height, 6; width, 9; depth, 2 mm.; Sta. 65;
Pal. Res: Imst., No. 6026.

Nuculas(sp2 ee = a Se
eLeft valve if a Nucula: height, 3.5; width or length, 5;
depth, 1 mm-; Sta. OI-J-113, ““Float’’; Pal. Res. Inst., No:

6027.

~]

Sreleptodomiu'sye sue ie hii © lente isc eeeeeenee eee ene een, AE
Left valve: height, 19; length, 62; depth, 4.5 mm.; Sta.
OWI Shoat alse hesselnst-e Non O02S.

9. Platyostoma ventricosum (Conrad) — ce c Peet. 76
Ileight, 25; width, 56 mm.; showing flattening of whorls
above; Sta. 63; Pal. Res. Inst., No. 6029.

10. Platyostoma ventricosum (Conrad)

The same specimen showing shape of whorls and size of
mouth.

11, 12. Platyostoma ventricosum, var. permundum, n. var. 76
Holotype: height, 25; width, 50 mm.; Sta. 63; Pal, Res,
Inst., No. 6030.

Buuu. AMER. PALEONT. No. 108, Pu. 8

PL. 34, VOL. 27

PLATE 9 (35)

4 BULLETIN 108 362

EXPLANATION OF PLATE 9 (35)

lrigure Page

1. Platyostoma ventricosum, var. permundum, n. var. : ei)
Same specimen as figs. 11 and 12 of Pl. 8.

2. Platyostoma neveritanum Weisbord - wal: == ee 76

Height, 20; width, 28 mm. Somewhat less spherical than the
specimen by Weisbord (Bull. Amer. Paleont., vol. 11, pl. 41,
figs. 1-3). Sta. 42; Pal. Res. Inst., No. 6031.

3. Platyceras sinistrum, n. sp. — eek a pita ehs a: ea. 17
Holotype: greatest dimension as shown in fig. 5, 40 mm. Note
how tue beak, as viewed from above, seems to turn toward
the right, while im fig. 1, the beak turns to the left. Sta. 72;

Pal. Res. Inst., No. 6032.

3a. Platyceras sinistrum, n. sp.
The same specimen viewed laterally, showing ‘‘umbilical’’ de-
pres ion demareated by a somewhat sharp ridge.

1. Platyceras? gibraltar, n. sp. E - : 2.25 2h
Holotype: viewed from above; Sta. 42; Pal. Res. Inst. No.
6033.

5. Platyceras? gibraltar, n. sp.

The same specimen as fig. 4; height, 30; length, 60 mm. Shell
mostly removed, thicker posteriorly than anteriorly, fine irregu-
lar radiating markings shown on cast of interior.

6. Platyceras? gibraltar, n. sp. ee ae ae (7
From the same specimen at ‘‘a,’’ showing irregular tubules
and perforations on what seems to be remnants of the inner-
most layer of the shell; perhaps a lichenaha-lke growth on
the inner surface of the shell after death of animal.

7. “Foraminifera” - Pens ee eran : a Lae 25
SSighinniny serena 8 iOS Shee, 155 Permo-Carboniferous. ’’—
Liddle. Pal. Res. Inst., No. 6034.

95

meuts and eardinal area of a Spirifer. Sta. 15; Permo-Car-
aE

boniferous. ’’—Liddle. Pal. Res. Inst., No. 6035.

Pu. 35, VOL. 27 Buu. AMER. PALEONT. No. 108, Pu. 9

PART Il. PALEONTOLOGY

B: ANTHOZOA
By
John W. Wells

The Ohio State University

In 1926 Weisbord described and figured three species of corals
from Devonian rocks in the upper course of Rio Cachiri, State
of Zulia, northwestern Venezuela. More recently another small
collection of corals was made by R. A. Liddle. These corals are
of considerable interest because of their close relationships with
the more or less well-known coral faunas of the Ulsterian and
IXrian stages, more particularly the former, of the eastern United
States and Canada.

During the course of examining the new material, it became
desirable to review the earlier material described by Weisbord,
and these notes present the results of a study of both collections.

live species, including as many genera, are recognized, prob-
ably representing a mere sample of the actual coral fauna of the
Rio Cachiri beds, This fauna seems to be the homotaxial equiv-
alent of the coral assemblages of the Ulsterian Onondaga-Colum-
bus-Jeffersonville formations of the United States and Canada,
but its facies, however, is not the more or less pure limestones
with coral bioherms of these units but rather that of the Ludlow-
ville formation (Irian) of central New York—arenaceous cal-
careous shales indicative of shallow, muddy bottoms, with corals
rather thinly scattered, and rarely growing luxuriantly enough
to build up bioherms or biostromes because of the influxes of mud.

Subclass RUGOSA
Ieliophyllum halli Milne Edwards and Haime, 1850 Plate 10, figs. 1, 2
(For partial synonymy see: Fenton and Fenton, 1938, p. 211.)
Locality and material.—Nine specimens, one of them figured,
from localities 36, 65, 72, 73, and 37.
Remarks.—Vhe specimens appear to represent typical H. halli,
with no notable variations from normal specimens from the

OG BuLLETIN 108 564.

Ulsterian and Erian stages in New York, Ontario, and Ohio. One
or two may represent an approach to H. — sciotoense Stewart
(1938, p. 39, pl. 7, figs. 3-5) although the distinctness of this spe-
cies may be questioned. The specimen figured has 84 septa at
the plane of the thin section about 15 mm. below the rim of the
calice with a diameter of about 33 mm. The primary septa of
the same specimen show only a very slight dilatation in the tabu-
larium, but in another one of the same size they are sharply
dilated in the tabularium and in nearly half of the dissepimentar-
ium. In radial section the dissepimentarium consists of the
usual dissepiments, while the tabularitum, composed of weakly de-
veloped tabellee, shows no distinct axial and periaxial zonation.

This species has already been reported from the Rio Cachiri
series of Venezuela by Liddle (1928, pp. 98-99).

Synaptophyllum vermetum (Weisbord) Plate 10, figs. 3, 4

Diphyphyllum vermetum Weisbord, 1926, Bull. Amer. Paleont., vol. 11,

De 220, pla 30, ties G5 ie: Dies Ope tl one:

Localities and material—Syntypes from upper course of Rio
Cachiri, State of Zulia, northwestern Venezuela. One large
colony, with nearly completely flattened corallites from locality 63.

Description.—Corallum phaceloid, with long, slender, flexuous
cylindrical corallites with somewhat annulated sides, frequently
touching each other but lacking radiciform processes. Diameter
of corallites ranging from 2.5 to 4.5 mm., averaging about 3 mm.
In transverse section there are about 44 subequal septa, with little
or no differentiation into major and minor septa except in the
early stages of rejuvenated corallites. They extend inwards less
than one-half the radius, usually nearer one-third. The inter-
sections of the dissepiments appear as a sort of wall near the
periphery. Peripheral parts of the septa carinated, but the car-
ine are often absent in parts of the corallum where the septa are
very short. In longitudinal section the dissepiments are horse-
shoe-shaped and form a single peripheral series. The tabule
are mostly complete, flat or slightly arched, with occasional in-
complete tabule near the dissepimentarium. Calice and_ septal
margins unknown.

365 Rio Caciirt Fossins: WELLS Q7

Remarks.—Vhe foregoing is a revised description of this spe-
cies based upon the new material and Weisbord’s type specimens,
from one of which transverse and longitudinal sections were cut
Geitre, nes, 3) 2) ae As-thuseredeimed, this coral: is-seem to, be
very closely related to the North American Ulsterian species, .S’s
simicoense (Billings), (vide Stewart, 1938, p. 43, pl. 8, figs. 5, 6)
in almost every detail except for the much shorter and practically
equal septa and lack of radiciform processes between the coral-
lites.

Ileterophrentis venezuelensis (Weisbord) Bence, U0); soKess 45 ts, &)
Cyathophyllum venezueclense Weisbord, 1926 Bull. Amer. Paleont., vol.

I ps 224, pl 30, hess 1-3:

Locality and material.—Syntypes from upper course of Rio
Cachiri, State of Zulia, northwestern Venezuela. Seven speci-
Mens trom localities: 36,537, 63, 72; and ]73.

Description.—Solitary, corallum conical, nearly straight in
early stages and strongly curved in large specimens. [pitheca
moderately thick, ridged, with low growth annulations. Calice
circular, slightly oblique, deep, with broad, nearly flat, raised
tabular floor. Number of septa in ephebic stage uncertain but
at least 100 in specimens 45 mm. in diameter. In a smaller one
there are 76 at a diameter of 25 mm., in two orders: larger ones
that extend more than two-thirds of the distance to the ,center,
and shorter ones that exend less than one-third. Deep in the
corallite the primaries extend to the center where they may be
somewhat twisted together, I ossula well developed, apparent-
lv on the side of greater curvature. Tabule numerous, more or
less complete in ephebic stages, convex, warped downwards
sharply peripherally, somewhat as in Siphonophrentis, closely
packed. In early stages they are very irregular and contorted.
Dissepimentarium formed by a rather broad zone of concentric
vesicular dissepiments. Peripheral stereozone well developed in
practically all specimens, extending at least to the ends of the
secondary septa and often beyond them to the inner margins of
the primaries in some cases.

O8 BULLETIN 108 566

Remarks.—More than one species may be involved in the
specimens included here, but no attempt to differentiate them is
practicable until more material is available. The species is very
closely allied to both H. prolifica (Billings) and H. spissa (Hall),
Hoth common North American Ulsterian species. The internal
structure of these has not been described adequately, although
sections of H. prolifica from the Columbus formation of central
Ohio examined by the writer are practically identical with
ephebic H. venezuclensis. There is also considerable similarity
with H. simplex (Hall) of the New York Hamilton group,
(nian \s (arde Elall 1876, pla2zir. ties,.7, 1h).

Zonophyllum, sp. Plate 10, figs. 5, 6

Locality and material—QOne poorly preserved specimen from
locality 73.

Remarks.—TVhe single specimen of a cystiphyllid coral is too
poorly preserved to be adequately described at this time, although
it is probably new. The form of the corallum, which 1s appar-
ently solitary, is irregularly cylindrical, about 12 mm. in diam-
eter, with irregular constrictions, some of which are the effect
of rejuvenation. In transverse section, there is an irregular
outer zone of small dissepiments on which the septal rays (about
100) are highly developed and heavily thickened by stereothecal
deposits. Centrally the cysts formed by coarse dissepimentlike
tabule often bear some septal rays. In longitudinal section, the
dissepimentlike tabulz, which are usually thickened by sterome,
form a central zone which in places extend nearly across the
corallite.

The genus Zonophyllum Wedekind, 1924, occurs in the lower
Middle Devonian of the Eifel region and has not hitherto been
recognized in America, but among the American Devonian spe-
cies of “Cystiphyllum” there occur forms very likely referable to
it; for instance, C. conifollis Hall (1876, pl. 30, figs. 3-9) of the
Hamilton group which has a growth form and structures (vide
Fenton and lenton, 1938, p. 232) similar to those of the Vene-
zuelan specimen.

367 Rio Cacnirt losstis: WELLS 99

Subclass TABULATA
Thamnopora venezuelensis (Weisbord) Plate 10, fig. 10
Pleurodictyum venezuelense Weisbord, 1926, Bull. Amer. Paleont., vol.
ik, jie BAG, joll ox), mies, ts, 8),

Locality and material.—Holotype from the upper course of Rio
Cachiri, State of Zulia, northwestern Venezuela.

Remarks.—Weisbord’s original description is inadequate, and
the following is offered in amplification:

Corallum small, apparently nodular and similar in form to
that of Favosites forbesi, the holotype being about 27 mm. in
height with a maximum diameter of about 17 mm, Basal epitheca

5 /
present, according to Weisbord. Corallites prismatic, diverging
regularly from the axis of main growth, ranging in diameter from
I to 1.5 mm. Calices only partially preserved, but apparently
more or less circular rather than polygonal. Interior of corallites
heavily thickened by stereotheca, through which the large
(0.25-0.3 mm.) single series of mural pores persists. Tabulz
complete, flat, averaging slightly less than 1 mm. distant from
each other.

The growth form of this species is not certainly nodular, and
the holotype may not represent a single colony, but may, instead,
be a stubby proliferation from a ramose corallum, In all other
respects it is closely related to 7. limitaris (Rominger) and T.
cariosa (Davis) of the Ulsterian of the northeastern United States
and Canada.

REFERENCES

Fenton, C. L. and Fenton, M. A.
Heliophyllum and ‘‘Cystiphyllum,’’ corals of Hall’s ‘*Illus-
trations of Devonian corals.’’ Carnegie Mus. Ann., vol. 27,
1938, pp. 207-250, pls. 17-24, 22 figs.

Htall J,.
Illustrations of Devonian fossils; corals of the upper Helder
berg and Hamilton groups. Geol. Surv. New York, 1876, 39 pls.
(with letterpress but no text).

Weisbord, N. E.
Venezuelan Devonian fossils. Bull. Amer. Paleont., vol. 11,
1926, pp. 223-268, pls. 35-41.

Stewart, G. A

Middle Devonian corals of Ohio, Geol, Soc, Am., Special Paper,
No. 8, 1938, 120 pp., 20 pls.

100

Pees ia
Mourne

1,2

ye

10,

3ULLETIN LOS

EXPLANATION OF PLATE 10 (36)

Heliophylium halli (Milne Edwards and Haime)
1, NIM; fie. 2, radial longitudinal

ig. 1, transverse section
section; X11.

Synaptophyllum vermetum
Figured syntype. Fig.

(Weisbord)

3, transverse section,

X6

wall and septa pertain to rejuvenated corallite) ;
longitudinal section (shehtly diagonal); N6.

Zonophyllum, sp.

Fig. 5, transverse section, X2; fig.

section, X11% (rejuvenated near middle).

Heterophrentis venezuelensis (Weisbord)
ig. 7, longitudinal polished section of figured syntype,

X1; figs. 8, 9, transverse scctions of hypotype;

Thamnopora venezuelensis

Longitudinal polished section of holotype;

(Weisbord)

X2.

All specimens are in the Paleontological
>

Researeh

Institution

(inner
fig. 4,

6, longitudinal polished

X1M%.

98

97

99

No. 108, Pu. 10

Buu. AMER. PALEONT.

PL. 36, VOL. 27

poges

Note:-Light face figures refer to
of the separate bulletins.
plate numbers.

A
Acharax

Acila isthmica burica 14

Acrospirifer olssoni
Actwon breviculus

INDEX TO VOLUME XX VII

WT

284, ;

STAINS eee
schencki < oe
Actinopteria sub-
ulrichi 34 284, 318,
Aesopus (Glyptzopus)
Alvania bartschi —— 24
oldroydae ;
Amphicyrtoceras ?
abruptum 129,
subeancellatum
Amphigenia elongata var.
weisbordi Sp) Real. BT Bian
Ancistrosyrinx cedonulli
reevl Pept aa allcrey,
Anomia peruviana
Antillophos
Arca : ean
Area (Argina) brevi-
frons pA ee Lee
(Scapharca) charcoazu-
lensis cae ft: aa Soe
(Seapharea) charcoazu-
lensis 16
(Scapharca) concinna
(Seapharea) emar-
ginata bata
(Cunearea) esmeralda
(Cunearea) nux 169,
(Seapharea) obesa
(Scapharca) wheeleri
Architectonica
OPSULES eee aeEeE 169,
Armenoceras subverte-
bratum 25. 1153
vertebratum 128,
Athyris spiriferoides
33 284, 318,
Atrypa reticularis
var. harrisi BYPASS ee
Aviculopecten, sp.
?Aviculopecten yeakeli
epee et ES eee een y 314,

B

Barbatia (Acar) illota

the volume paging and not to the paging

Heavy face figures refer

172

130
131

338
323
334
284
284
341

161

3erry, S. Stillman on
Pleis ocene Mollusca

Bivetopsis

3orsonella
agassizil
(Borsonella) 25
adamsi
ephigonia
harrisi 25

Buridrillia
panarica

3ursa nana
var. jamanensis

Cc

Calearata

Calyptrogena pana-
mensis

Camaroteechia, sp. 32

Campo Chico formation

Cancellaria sp.

Cancellaria (Peruclia)
bulbulus

centrota

charapota
colombiana 22
(Cancellaria) ef.
decussata

(Eucla) pacifica
(Calearata) peninsul-
aris

(Cancellaria) penita
(Calearata) peninsul-

Giese ee 24
(Cancellaria) penita

21
(Charcolleria) perdi-
ciana : 21
(Charcolleria) terryi

21

(Cancellaria) urceo-
lata
(Cancellaria) ventri-
cosa 2
Cano del Oeste
formation
Cano Grande forma-
tion :
Cantharus amycus 24

369

to the

167,

170,

284, :

168, 170,

17

4,

volume

elegans :
Cardita laticostata
Cardium (Fragum)
magnificum
(Trigoniocardia)
vale

obo-

(Mexicardia) procerum
(Trigonioecardia) spiek-

eri ed ee
Cedarvilloceras —_-----
Chama (Echinochama)
ealifornica
corrugata
Charcolleria :
Chione (Chione)
amathusia
araneosa
cancellata
(Lirophora) ebergenyi

ef.

16

(Lirophora) kelletti

marie

subimbricata

(Chione) vaca

Nees ps 18
Chonetes sttibeli 32
Chonetes subhemis-

pherica . ols BY

venezuelensis _— 32
Circulus, sp
Clathrodrillia

amr Sil. ee
Clathrodrilla (Buridril-

lia) panarica 20 167,
Clathurella canfieldi
conradiana
cymodoce
tridesimilae
Cogollo formation
Columbella major
Condylocardia pana-
mensis
Conocardium
Conus arcuatus
(Leptoconus )
atus NE AR
gradatus - eee
imitator lius ef.
patriceus
planiliratus
puncticulatus
pyriformis
regularis
Corbula ovulata
(Varicorbula) cf.
bradleyi
granti et

16

719

15

VoLUuMs XXVII

170,

162,

169,

UPA,

IGE), Al

169, 171,

cacumin-

ITAL,

170,

172,
170,
Pals

167,

Coryell oN. meen =

Cotonopsis
Crassinella, sp.
Crassaspira, sp.
Crenella ecuadoriana
Crepidula onyx - :
Crucibulum (Crucibu
lum) hispidium
Ctenodonta?, sp.
Cyathophyllum venezu-
elense
Cycloceras
Cymatophos galerus
panamensis
Cymostrophia
Cyprea alabamensis
albuginosa
amandusi
annettze
annulifera
arabicula
ballista : 8
bayerquel
carolinensis
carolinensis flori-
danus : : 8
castacensis
cayapa
cervinetta
cervus : ;
chilona _ 8
cinera
eosmithi
estellensis
fresnoénsis —
gemmellaroi
healeyi et SEG
ed) r iri 9
hemisphaerica
henekeni
henekeni
henekeni
isabella
isabella
isabella
kempere
kennedyi
lapidosa
ludoviciana
mathewsonii
merriami
mortoni
mus :
nigropunctata
novasumma
nuculoides
oakvillensis

amandusi
poteronis

mexicana
patrespatriae
9

oC

Woe

379

1

(yA5 Alifil,,
169,
161,

Sie
99);

99,

98, 109,

Ste

99
110
99
99
105
105
105

INDEX

pilsbryi 9 105
pinguis : eng 105
sabuloviridis 109, 110
Se mente 5-2 ee 101
SIME NISIS) Hee es 9 105
sowerbyi —_...... 99, 107
spadicea fon 28, 107
squyeri 10 98, 106
spheroides 10 106
suciensis 98, 106
tithonica 98
trinitatensis att 99
tumulus 10 106
vaughani 10 106
willeoxi pee LO 106
Cypredia 108
chira 97
fenestralis | 11 97, 109
kugleri 3 = 97
subcancellata 11 97, 109
vistabellensis aes 97
Cypropterina pustulata 173
Cyrtoceras ? cancellatum 130
lentigradum 64, 65
simplex 67
Cyrtorhizoceras 141
camurum oi Pe. S 68
coralophilum ____ 12 145
filiferum 12 145
filosum ot 68
reimanni fece 1183 143
D
Dalium ecuadoriana 22 229
solidum _— 229
Dall, W. H. ee 175
Dalmanella sp. - oi) 324
Dalmanella cf. nettoana 284, 318
Dawsonoceras te 134
americanum 12, 128,129, 137,, 139
annulatum 1305 135. 139
annulatum ameri-
canum a 139
graftonense 137
hyatti 137, 138
jompbUhelramehebheeh 138
nodocostatum LSD los
percostatum 141
rugosum 137
senescens SA
tenuilineatum 135
Deiroceras curdsvil-
lense 56
dismukense 56
Deirosteus 261
abbreviatus 263
Deltoceras vaningeni 34

$71

Dentalium, sp. E
Dentalium (Fissiden-

talium) buricum 19
esmeraldum 19
Dentalium granadum _.

Diphyphyllum verme-
tum
Dictyoclostus lid-

dlei __ : 32
Dictyostrophia

cooper = == 30
Diestoceras ? sp... 4
Diplodonta, sp. :
Discosorus conoideus
Distorsio decussatus
Divaricella lucasana
Dosinia (Dosinidia)

FREE MIIIS,

E

Edmondia sylvana 34
Ellesmeroceras }

bridgei Po 83

expansum 3

foerstei

Scheie a es a
Elytha colombiana — 33

plana yen eee 33
EKodevonaria —.____ Ae
Eodevonaria imper-

alis : oy.

subhemispehrica
Epitonium (Ferminos-

cala) ferminianum 22
Eucrassitella gibbosa
Eurystomites kellogi

F
Favosites forbesi
Fenestella venezue-

lensis) 2 = werk
Ferminoscala
Ficus ventricosus
Fissidentalium
Fissidentalium buricum

Flower, R. H., on Seward
Peninsula cephalopods
on cephalopods from
the Cynthiana of Ken-
tucky ; :
On Clinton cephalo-
pods

Fusinosteira

Fusinus sp.

Fusinus mellissus,
neesps

bo
NS

284,

513,

318, :

318, :

panamensis
IFusiturricula fusi-
nella shes Nh
woodringi 20
G
Gayuta group
Gayuta shale
Geisonoceras wauwa-
tosense

Gisortia clarki _. 11
Glyphostoma trides-
mia il

Glyptaspis abbrevi-
ata ee a rele ba t

Hanetia (Fusinosteria)
alternata - 7253
Hanetia anomala
burica = 2 24
elegans sriiand es
pelicaniage een G
Harpe SP. a
.eliophyllum
halti Sis esi, cals.
sciotoense
Heterophrentis
prolifica
simplex
spissa
venezuelensis

36, 283, 313, 314, 318, ;

Holonema
eifeliense
horridum
ornatum
radiatum
rugosum = 740

Inachus undatus
Ingram, W. M.
On type fossil

Cypreidze

K

Kionoceras mutabile

perlineatum 13
rochesterense
strix ; —
subcancellatum

L

Labiosa undulata
La Luna formation
Lamelliconcha
Latirus, sp.

penitus Be 74h

168,

314,

VOLUME XX VII

218 WENGICORIS 222 ee
Lechritrochoceras

167 bannisteri
167, 205 clintonense.._ 12, 13
notum

waldronense

a Leptena boyaca ____
: Leptena rhomboi-
ie dalis ew oO
ie 0 Leptodomus Yeoh te
a ulrichi : 34
Leptrostrophia carib-
8 beana _ 30
P concinna nel
261 ef. conecinna _... 30
Leucosyrinx buri-
canary == " 25
171, 219 nicoya 25
; ealapagana
169, 219 Persimilis

218220) -aecoya
174. 21g ULeurocycloceras
168 bucheri

clavatum
320, 363 niagarense
364 raymondi Be
ringuebergi eli
266 rochesterense

366 Liddle, R. A., Cachiri
366 section ss ——
Limoptera tenuis 34
99 29e5 Lirophora Pa
aoe gee Lirularia aresta 1
264 Longitrella
264 Lucina (Lucinoma) 17

264 aequizonata
264 acuwtilineata
261, 262 annulata
ches chiripanicus
heroica
28 Luciploma panamen-
sis re 16
M
95 Macaliopsis
Macoploma SE
oo io Macoma (Panacoma)
132, 133 chiriquiensis 18
; 133 Macoma (Macoploma)
130, 133 medioamericana 17
: 134 Macrocallista, sp.
130, 133 Maerocallista auran-
tiaca
pannosa
ae squalida
189 traftoni 18

172 Melonoceras’ reclinatum
Melonoceras ? re-
clinatum

284,

284,

ill

142,

318,
313,
284,
318,

167,

129,

319,

167,

174,

167,

173,

217
146
148
147
148
147
317

325
201
343

325
284
325

209

Marginella
sapotilla
Megaloplax marginalis
Meristella, sp. 33
wheeleri 33
Metula_ sp. ——
Metula amosi 22
pilsbryi ey)

Michelinoceras 2 vi irgu-
latum :
Microglyphis schencki -
Misoa-Trujillo forma-
LENG Lae 2
Mitra belcheri_

cyclica 20
Mitrella (Longitrella)
vespertina 23

Mitromorpha aspera
barbarensis wood-
fordi - rane i 1
filosa
galeana
gracilior
interfossa 3

Modiolus ef. purpur-
atus -

Moniliopsis chacei 1
rhines
fancherae
ophioderma

Mossman, R. H.

Murex recurvirostris

N

Nassa (Arcularia) punta-
blancoensis
Nassa (Uzita) armu-
ella
miser
terryi
Natica broderipiana

21

169,
23

scethara burica
Nautilus jason __
Neumatoceras
carlsoni
Sip beTosumy se
Neetia reversa magma
Nuclearia gabbiana
madagascariensis
nucleus re
Nucula; sp. 22
agapea
iphigenia ae
iphigenia azulensis —
le(e

34

284,
284,

170,

161,

IETIbs ¢

168,

UGG, Io alias alge.

INDEX

Nuculana (Jupiteria)
chiriquiana
davidiana

14

14 167, 172,

O
Oenopota fidicula
turrispira 2 1
Oliva angulata
araneosa
spicata
(Agaronia)
venulata x
Olivella, sp. _—
Olsson, A. A. _
Ooceras
Oocerina
shamattawense
Oonoceras
ACwnMN =)
brevidomum
gracilicurvatum
graciliforme
multicameratum 6
obstructum
planiseptatum
shamattawense
subcuneatum ae
suborthoforme - 4
subrectum ees nee
triangulatum 7
triangulatum cylindra-
COIN 4
wyomingense
Ormoceras ? coving-
tonese
lindsleyi
troosti
Orthoceras annulatum
annulatum americanum
duseriy == 55,
imbricatum
undulatum
virgatum ?
Ostrea, sp. :
Ostrea megadon :
Oxygonioceras simplex

1p

Palmarito series -

Banacomay =" 2s aeanee

Pandora (Clidiophora)
Spo =

Pecten dentatus
tumbezensis

Malea ringens

Margarites aresta 1

testacea 169, 170,

50,
4, 5

163, 171,

167,179

180

ial
173
13

ventricosus

Pentagonia
gemmisuleata 33
unisuleata

Periploma lucina 16
periscula
planiuscula 169,

ef. stearnsi
Permo-Carb.-Creta-
ceous relationship
Mesozoic
Phacoides liani
Phos (Antillophos)
watunensis
mexicanus
HUtSChil 2208 16O wiles.
Phyllonotus brassica
Phymorhynehus
Pinna sp.
Pitar (Pitarella)
Pitar (Lamelliconcha)
anona 18
concinna
mellisa
rosea q
Placunanomia, sp.
cumingsii
panamensis
Platyceras gib-
raltar
sinistrum 35
Platyostoma neveri-
tanum
ventricosum
ventricosum var.
permuudum
Plectoceras
carletonense
foerstei
halli
jason
landerense
lowi
occidentale
sewardense 3
tyrans
undatum
Pleurodictyum vene-
zuelense
Pleurotoma
dissimilis
Pleurotomella argeta
Pleurotomella (Phymor-
hynchus) agina 23
Plicatula dubia
Polinices sp.
(Neverita) glauca
(Polinices) ef. pana-

18

vedonulli

VOLUME XXVII
161 mensis pase 172, 173
aff. reclusiana 175
284, 339 cachirita PAVE Bula alee Billy, Bulk)
318 Polystira, sp. 170
184 panamensis 25 167, 202
184 Productella, sp. 32 284, 318, 333
171, 172 Productus 332
Neil, alesis) liddlei 313
Pseudamusium pana-
mensis 167
294 terryi Se 167, 182
169 R
174. 224 Rhipidomella liddlei
J 995 ae ci 30 284, Silos 20 oes
178, 225 Rhytistrophia carib- we
169 beana 325
208 Richardsonoceras 142
161 clarkei 68
171 falx 68
romingeri 68
169. 189 schofieldi 68
471 simplex 68
169, 189 3 subcuneatum 67
170 wyomingense —____ 67
171 Ringicula (Ringiculella) :
184 costaricensis ; 19 il'7fal., 231
162. 183 Rio Cachiri section 27 321
: Rio Guasare formation 303
314. 345 Rio Negro formation 295
984. 345 Rizoceras : 60
maa carletonense 52 ae
344 conicum 4 ‘ 61
317. 344 coronatum bye (5)
¥ graciliforme 5 52: Ole 62
317, 344 S
28 Sanguinolaria
29 (Sanguinolaria) azulen-
PA. | Bal sis 18 167, 194
29, 34 San Pedro Pleistocene 3
29 Secapharea charcoazulia 167
29 Schellwienella
29 goldring2x 30, 284, 313, 318, 326
29 Schizodus venezue-
QAS oe, lanus 284
29, 35 Shark’s tooth 284, 318
29 Sierra de Perija se-
ries 278
367 Siphocyprea problem-
205 atica 10 97, 107, 108
208 Siphonalia? 174
167, 209 Siphonophrentis 365
Skenea ? cyelostoma 1 14
167, 208 Skenea planorbis 14
161 Solemya (Acharax)
174 burica 15 i07 (5)
172 Solenosteira alternata 219
Spirifer mesacostalis 262
sp. 311

374

Spiriter oe 19 Rde 39.
kingi 535) ESV Shik
olssoni aa) Pasyil Bull.

Spirifer weis-
bordi a, oy ASL BUI

Strigilla, sp.

Strioterebrum

Strombina (Cotonop-
sis) sp.

Strombina ecuadori-
ana TOS 2;
fusiformis
penita 23 226, 169,
recurva 169, 170,

Strombina (Cotonop-
sis) panacostari-
censis PB

Strombinophos loripana
loripanus 169, 170,

Stropheodonta (Cymostro-

phia) casteri all 284318)

kozlowskii 284,
Strophonella? meridion-

alis 3 284" 33,
Sulcocyprea lintea 10 97,

Surcula nelsoni

Synaptophyllum simeco-
ense : :
vermetus BH Bassey) aiillel,

Tagelus (Mesopleura)
peruvianus

Talityphis

Tarphyceras culticam-

eratum __

Tellina (Eurytellina)
ecuadoriana
(Macaliopsis) fron-

tera : Ease) iNet.
(Eurytell ina) pana-
manensis ae
Tellinopsis venezuel-
ENO, ae 34 ara
Tellinoyma 34
Terebra armillata
Terebra (Striotere-
brium) sp.
Terebra (Strioterebrum)
aspera Z LOO 2.
(Strioterebrum)
eracilenta 2Ae AO 2s

(Terebra) elena
(Strioterebrum )

guanabana 24 169,
(Terebra) lingualis

luctuosa

Strioter ebrum)

panamillata —_ 24

|

314
336
336

Bon
ial
198

168

173
220
171
173

22
168
172

327
318
327
108
207

364
364

172
228

31

NDEX

(Terebra) robusta
sheppardi
(Strioterebrum )
vaca

Terry, R. A.

Thais cf. biserialis

Thamnopora cariosa
limitaris
venezuelensis 36

Thracia (Cyathodonta)
dubiosa
undulata

Thyasira bisecta

Treptoceras
milleri
perseptatum
persiphonatum
prenuntium

Tritiaria (?) ecuador-
lana

Tropidoleptus cari-
natus opts PRE Bey

Turricula astia)
andesita 20
duleia, n. 20
flammea
libya

Turritella gatun-
ensis
tigrina

Turris fusinella

Typhis (Talityphis)
costaricensis

Typhis martyria

24

15

4,

aes

(Knef

sp.

bo
wa

Uzita
Vv
Varicorbula
Virgoceras
Vitularia cf.

cancellatum
salebrosa

Ww

Wells, John W.
On Holonema from Up-
per Devonian of New
York 2
On Rio Cachiri
corals

Y
Yoldia panamensis
Yoldia (Orthoyoldia)
quiba 16
Z

Zonophyllum

Zonophyllum, sp. 36

~I
un

999

197
136
170

oF VoL. XXVII

376

Aaa

ty eer)

Hn ni fi i We

7. } rh i) ] , itp on RY
t ; UN wie i vie
ih th shy) ‘HK Nyt Pay CAN } "i Hav ia bin us
{ eat i wit } hpi iW cy }
ie Dif ; he
iy
HYD

a

H i Mi A vie ir f

Mf ee se ir

ee rr a eke

OE gt eae
ee

tot Fen ets
Mn gti TE

FEEDS Pw Bre
2 ae ee ny parent
icpicsticheh-an gt capes gaan

aet/
OO By aet 2e epee Rigg ae See

ne Sindee

peagta reas
Sean abeaty Prey a
: at ee ict

See Rees

t= nbeaetohe tie
ANTS

nee enn bhatt
ters ep OE

ee ewe
See cee ee ere :
np gempn rt E gee we a Gack me “ is
oa Seetncaaeratden dee anion 3 « ane
Sn te ring Pew ‘ i ;

a lekcod une Maite teks eee Bm iy Aen oi ‘“ -
er smh mene oy te a em : - vie as ota oe
‘ mee : vs ones - i detumnbeieadamntt aman a
Pe Sty eh tamer

emnorens