UC-NRLF
C E fl?l SD1
University of Texas Bulletin
No. 1X56: October S.
The Weno and Pawpaw Formations of the
Texas Gomanchean
IIV
W. S. AdVins
\
On A New Ammonite Fauna of the Lower Turonian
of Mexico
BY
Emil Hose
Bureau of Economic Geology and Technoli gy
Division of Economic Geology
. A. Udden, Director of the Bureau and Head of f ?ie Division
PUBLISHED BY
THE UNIVERSITY OF TEXAS
AUSTIN
EARTH
SCIENCES
LIBRARY
51520 9«04818-2m
University of Texas Bulletin
No. 1856: October 5, 1918
The Weno and Pawpaw Formations of the
Texas Gomanchean
BY
, . ' . - . •
•: ; '.' ,
W. S. Adkins
On A New Ammonite Fauna of the Lower Turonian
of Mexico
BY
Emil Hose
Bureau of Economic Geology and Technology
Division of Economic Geology
J. A. Udden. Director of the Bureau and Head of the Division
PUBLISHED BY THE UNIVERSITY SIX TIMES A MONTH, AND ENTERED AS
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UNDER THE ACT OF AUGUST 24, 1912
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The Weno and Pawpaw Formations of the
Texas Gomanchean
BY
W. S. Adkins
CONTENTS
INTRODUCTION 9
STRATIGRAPHY 13
Rocks underlying the Weno and Pawpaw Formations
Pre-Comanchean *"
Comanchean *4
Thickness changes
Lithological changes
Weno and Pawpaw Formations
Thickness changes 25
North-South changes 25
East-West changes 26
Lithological changes
Pawpaw Formation >
Weno Formation 35
Stratigraphic Correlation 40
North Central Texas and Southern Oklahoma 40
South Central Texas 40
West Texas and Mexico 41
Europe and North Africa 4 a
PALEONTOLOGY 44
The Weno Fauna 45
The Pawpaw Fauna 4?
Comparison of Pyrite Faunae 53
Texas 53
Kiamitia Clay Fauna 54
Duck Creek Marl Fauna 64
Denton Clay Fauna '. 55
Grayson Fauna 5(5
Del Rio Clay Fauna 58
Summary of Pyrite Faunae 60
Europe and Africa
DESCRIPTIONS OF SPECIES 68
CEPHALOPODA 68
Nautilus texanus Shumard 6S
Nautilus sp
Hamites tenawa Adkins and Winton 69
Hamites sp. aff. armatus Sowerby
Ancycloceras bendirei n. sp '"
Hamulina wortkensis n. sp
Baculites comanchensis n. sp ?4
Turrilitcs bosquensis n. Sp
Turrilites worthensis Adkins and Winton 78
Turrilites sp
Scaphites hilli Adkins and Winton 79
6 University of Texas Bulletin
Engonoceras serpentinum (Cragin) 8-1
Engonoceras sp 85
Flickia boesei n. sp 85
Flickia (?) bosquensis n. sp 87
Schloenbachia wenoensis n. sp 89
Schloenbachia wintoni n. sp 90
Mortoniceras worthense n. sp 91
Acanthoceras worthense n. sp 93
ASTEROIDEA , 95
Pentagonaster texensis Adkins and Winton 95
Metopaster hortensae Adkins and Winton 97
Comptonia wintoni n. sp. 97
Pentaceros americanus n. sp 99
ECHINOIDEA 101
Leiocidaris sp 101
Goniopygus sp 102
Pedinopsis symmetries (Cragin) 102
Peltastes sp 102
Salenia sp 103
Cyphosoma volanum Cragin 103
Holectypus limitis Bose 103
Holaster sp. aff. simplex Shumard 104
Epiaster wenoensis n. sp 105
Epiaster aguilerae Bose 109
Epiaster subobesus n. sp : 110
Enallaster wenoensis n. sp 112
Enallaster bravoensis Bose 114
Enallaster sp. aff. texanus (Roemer) Hi
Hemiaster calvini Clark ; 114
Hemiaster riovistae n. sp 115
PELECYPODA *. H8
Nucula nokonis n. sp 118
Nucula wenoensis n. sp 120
Area washitaensis n. sp 121
Gervilliopsis invaginata (White) 122
Ostrea carinata ? Lamarck 122
Ostrea sp. aff. diluviana Linnaeus 122
Ostrea (Alectryonia) quadriplicata Shumard 123
Exogyra sp. aff. arietina Roemer 123
Pecten inconspicuus Cragin 123
Pecten georgetownensis Kniker 125
Venericardia wenoensis n. sp 125
Protocardia sp. aff. multistriata (Shumard) 126
Corbula wenoensis n. sp 127
Corbula basiniformis n. sp *. 130
Corbula littoralis n. sp ^33
Cyprimeria washitaensis n. sp 134
Remondia ? acuminata (Cragin) 13g
Weno and Pawpaw Formations
GASTROPODA 137
Amberleya graysonensis n. sp 137
Trochus laticonicus n. sp 138
Helicocryptua mexicnnus B6i»e 139
Nerita sp 139
Neritina sp 139
Anchura mudgeana White 139
Natica sp 140
Lunatia sp 140
Globiconcha sp 140
Turritella graysonensis n. sp 140
Turritella worthensis I), sp 142
Cinulia washitacnsis n. sp 143
PROTOZOA 145
Nodoiaria texana Conrad 145
BIBLIOGRAPHY 146
PLATES 1—11. . ..149-170
8 University of Texas Bulletin
LIST OF ILLUSTRATIONS
FIGURES
Figure 1. Map of Texas and part of Oklahoma showing outcrops of the Weno
and Pawpaw formations, and the lithological facies of the
Pawpaw formation 11
Figure 2. Ancycloceras bendirei n. sp., suture of the type individual, camera
lucida drawing, x 5 71
Figure 3. Hamulina worthense n. sp., sutures of type individual, camera lucida
drawing, x 15 73
Figure 4. Baculites conuanchentis n. sp., sutures of type individual, camera
lucida drawing, x 8 75
Figure 5. Turrilites bosquentis n. sp., sutures, type individual, camera lucida
drawing, x 8 77
Figure 6. Scaphttes hilli Adkins and Winton, type individual, diagrammatic
restoration showing orientation and sutures, camera lucida
drawing, x 12 82
Figure 7. Scaphites hilli Adkins and Winton, young individual, showing the
last five sutures, camera lucida drawing, x 10 83
Figure 8. Scaphite* hilli Adkins and Winton, external and internal suture,
camera lucida drawing, x 10 84
Figure 9. Flickia boeiei n. sp., type individual, sutures, camera lucida draw-
ing, x 8 v 86
Figure 10. Flickia bosquensis n. sp., diagrammatic projection of sutures of type
individual, camera lucida drawing, x 5 88
Figure 11. Schloenbachia wintoni n. sp., type individual, last suture, camera
lucida drawing, x 5. Keel region slightly distorted in type
individual r 91
• Figure 12. Mortoniceras worthense n. sp., suture of individual, Plate 1, figure 6,
camera lucida drawing, x 10 93
Figure 13. Acanthoceras worthense n. sp., suture, camera lucida drawing, x 8 94
PLATES
Plates 1 — 11. Fossils of the Weno and Pawpaw formations . .149-170
THE WENO AND PAWPAW FORMATIONS OF THE TEXAS
COMANCHEAN1
By W. S. ADKINS
INTRODUCTION
The Weno and Pawpaw formations are two thin formations lying near
the top of the Comanchean series of strata, and are most typically developed
in the region between the Red and the Brazos rivers. The importance of
these formations, especially the Pawpaw, is much greater than their thick-
ness would seem to indicate. The Pawpaw is a formation of small thick-
ness, sharply limited lithologically both above and below, and contains
a remarkable series of small pyritic fossils which are so sharply charac-
terized and so distinctive in appearance, even in minute fragments such
as are encountered in drilling, that this formation should be recognized in
wells lying to the east of its outcrop and should furnish at least one certain
and dependable stratigraphic level in the Comanchean. In the hope that
the formation may have this value, its fauna has been described in some
detail and the lateral variations in its lithological character indicated.2
The same statements hold to a lesser extent for the Weno formation. The
stratigraphic position of these two formations in the Comanchean series
and their equivalents in the Central Texas section are given in the fol-
lowing table.
The Weno and Pawpaw formations are visible over a small areal extent,
their outcrops aggregating somewhat more than 100 square miles, mainly
in a narrow strip in Johnson, Tarrant, Denton, Gooke and Grayson Coun-
ties, Texas, and Love, Marshall, Bryan and Choctaw Counties, Oklahoma.
In addition they have stratigraphic equivalents in Central and Western
Texas and in Mexico, that will be discussed later. Their north-south dis-
tribution in Texas is between Lat. 32°N. and 34°N. ; and their east-west
distribution is practically unknown. In Oklahoma their east-west distri-
bution is between Long. 95°15' and 97° ; and their north-south distribution
is unknown. The total length of their outcrop north of the Brazos River
'Manuscript accepted June 15, 1920, published November, 1920.
"It is hoped that operators and others having well samples suspected of being Upper
Comanchean will submit them for examination to the Bureau of Economic Geology
at Austin.
3I wish to express my indebtedness to Professor W. M. Winton, with whom the
preliminary work on these and other Comanchean formations was done jointly. The
results of these studies will appear in forthcoming papers by both authors.
10 University of Texas Bulletin
CORRELATION TABLE OF THE COMANCHEAN FORMATIONS OF CENTRAL TEXAS'
Series
Division
Formations
North of the
Brazos River
Formations
South of the
Brazos River
Stage
UPPER .CRETA-.
ofldya.: '
.'. ."' '. '-•'
Uagleford
Eagleford
TURONIAN
COMANCHEAN
WASHITA
Woodbine
Grayson
Mainstreet
Pawpaw
Weno
Denton
Fort Worth
Duck Creek marl
Duck Creek Ls.
Kiamitia
Buda
UPPER
CENOMANIAN
Del Rio
Georgetown
LOWER
CENOMANIAN
VRACONIAN
FREDERICKS-
BURG
Goodland
Walnut
Edwards
Comanche Peak
Walnut
ALBIAN
TRINITY
Paluxy
Glenrose
(Basement Sands)1
Glenrose
Travis Peak
APTIAN
PENNSYLVAN-
IAN
Unconformity
PENNSYLVANIAN
is about 110 miles in Texas and 100 miles in Oklahoma. The outcrop is S-
shaped, and north and west of its limits in North Central Texas the forma-
tions are eroded away; while east and south of the outcrop, the Weno-
Pawpaw rock sheet continues underground for an unknown distance, being
buried beneath the more recent Comanchean and Cretaceous strata. This
concealed extension of these formations still awaits exploration by means
of detailed well logs and the examination of samples from drillings. The
formations show distinct north-south changes along their outcrops and
equally distinct east-west changes. As a whole, they thicken moderately
from the Brazos river (near Blum) north to the Red River (north of
Gainesville) , and thence eastward down the Red River valley through Den-
'See also: Bose, University of Texas Bulletin, 1902, p. 16, fig. 1.
2The Comanchean sea was transgressive northwards over much of Central Texas,
and the Basement sand is not a single formation, but at different places is the time
equivalent of various off-shore formations.
Hi no and Pawpaw Formations
11
Fig. 1. Map of Texas and part of Oklahoma, showing outcrops of the Weno and
Pawpaw formations and the lithological facies of the Pawpaw formation.
SI— Sandstone and Ironstone; Cl— Clay; M— Marl; LS— Limestone.
12 University of Texas Bulletin
ison and Bennington they thicken rapidly ; so that by inference the main
thickening is ENE. and the lines of equal thickness run about 60° E. of N.
Southward from the Red River in Cooke County the Weno and Pawpaw
formations thin gradually to at least the Colorado River where they are
probably represented by strata lying near the top of the Georgetown lime-
stone. The two formations behave very differently over the area men-
tioned. The Weno formation, south of the change of direction of its out-
crop in Cooke County decreases slightly in thickness, from about 75 feet
near Gainesville to 65 feet near Fort Worth, 60 near Riovista, 40 near
Waco, and 20(?) near Georgetown. The Pawpaw clay on the other hand,
thins more rapidly from the Red River southward. Near Cedar Mills,
Cooke County it is 60 feet thick, in Denton County 40 feet, at the north
border of Tarrant County 27 feet, on Sycamore Creek near Fort Worth 24
feet, at the south border of Tarrant County 12 feet, at Riovista 5 feet, at
}Blum 3 feet, and near Waco about 2 feet thick. This thinning is a part of
the general thinning southwards of the softer formations of the North
Texas Washita, which south of the Brazos are represented in the George-
town limestone, as is observable in the Kiamitia marl, Duck Creek marl,
Denton marl, Pawpaw clay and Grayson marl. The alternate harder for-
mations, the Duck Creek limestone, Fort Worth limestone, Weno limestone,
Mainstreet limestone, undergo proportionately less thinning southwards
and hence contribute relatively larger components to the Georgetown lime-
stone.
There are equally distinct differences of lithology and facies, which are
presented later.
The present paper is only an introduction to the large and interesting
Weno and Pawpaw faunae, the majority of whose species are still unde-
scribed. Much collecting and further study is required before any attempt
can be made towards a monographic treatment of these fossils. It will be
noted that the limits set in this paper coincide with the boundaries of hori-
zons 25 to 33 inclusive, of Adkins and Winton's preliminary section of the
North Texas Washita division.1
1 Adkins and Winton, Paleontological Correlation of the Fredericksburg and Washita
Formations in North Texas. Univ. Texas Bull. 1945, 1920.
STRATIGRAPHY
The stratigraphy of the Weno and Pawpaw formations involves the re-
gional stratigraphy of the Comanchean area north of the Brazos River, and
accordingly, certain lithological and structural features of this region will
be described.
In almost the whole region in question, along the line of outcrop of these
two formations between the Brazos and the Red Rivers, the Comanchean
sediments are deposited over a large geosyncline whose axis is transverse
to the direction of the Comanchean outcrops — i. e., roughly northwest-
southeast — and whose bulk was largely filled in by pre-Comanchean depos-
its. However, there is a feeble surface reflection of this buried structure,
which influences the thickness and lithologic characters of all Comanchean
deposits, including the Weno and Pawpaw formations. The north edge of
this deep trough is near the. Red River and the south edge is south of the
Brazos ; the north slope is steep and the south slope more gentle. This de-
pression, in which the Fort Worth region is located will be called the Fort
Worth geosyncline.
ROCKS UNDERLYING THE WENO AND PAWPAW FORMATIONS
PRE-COMANCHEAN
Its extent may be indicated by the meager data available on the under-
ground position of the Ellenburger limestone. At Muenster, Cooke County,
it was reached at a depth of about 1800 feet, or 1050 feet below sea level.
At Myra, Cooke County, the Ellenburger was reached at a depth of 1640
feet below the surface or about -900 feet (sea level).1 In the Polytechnic
(Byrens-Burchell No. 1) well near Fort Worth, the Ellenburger if present
lies below -3950 feet, at which level the Bend has probably not been reached.
The difference in elevations of the last two subsurface points is 3050 feet
which represents the minimum change of elevation of the first Ellenburger
reached between Myra and Fort Worth, in case the Ellenburger is present
at the latter place. Coincidentally the thickness of Pennsylvanian deposits
is not more than 600 feet at Myra, but has increased to at least 3600 feet at
Fort Worth. Other wells in Tarrant and nearby counties have penetrated
similar Pennsylvanian material.
Farther south there is doubt that the Ellenburger is present. In the
Hillsboro well the pre-Cambrian rocks were said to be reached at a depth
'Matteson, Econ. Geol., XIV, No. 2, p. 1919.
14 University of Texas Bulletin
of 2100 feet, apparently without intervening Ellenburger, and at Waco
th,e pre-Cambrian is present at about 2500 feet. However, at points still
farther south and southwest, as at Gatesville and Leander, the Ellenburger
is present but thin, and overlies pre-Cambrian shales or slate-graywacke
which near Leander are stated to be identical in appearance with the
Virginia shales and to be of upper Huronian age.1 At Georgetown, Leon
Springs and Camp Bullis,2 the Trinity directly overlies the pre-Cambrian
schists;3 the depths of the contact are respectively 1100 feet, 1015 feet, and
1790 feet.
The depression which is triangular shaped and narrower to the north-
west, is flanked to the north, at least in Cooke County, by a structurally
high area of Ellenburger at -900 feet, and a thin Pennsylvanian ; and to
the west by the structurally high Bend Arch in which the -3000 and -3500
Ellenburger contours have a trend east and south.4 Whether this Ellenbur-
ger depression opens to the southeast or to the northwest is not known to
me. It was, however, invaded by the Pennsylvanian seas which deposited
in its central part at least 3600 feet of sediments, and left a surface which
was more largely levelled than the original floor.
Upon this surface the Comanchean sea transgressed from the southeast,
depositing sediments which still show a feeble reflection of the underlying
geosyncline.
COMANCHEAN
THICKNESS CHANGES
Any pre-Comanchean ridges and valleys over which the Comanchean
seas spread would be indicated by deposition which is thicker in the valleys
and thinner over the crests. If therefore we identified a regional thinning
of the beds in two directions from a given location, this might be attributed
to deposition on two sides of an existing valley in the ocean bottom, whether
originally this valley was erosional or synclinal. This lensing is evident in
the Comanchean formations, and particularly in the lower ones (Glenrose,
Paluxy) . For example the Glenrose fills in much of the depression by lens-
ing; at Decatur it is about 35 feet thick but at Fort Worth about 475 feet,
aBy Professor A. W. Johnston, oral communication.
2Sellards: The Geology and Mineral Resources of Bexar County, Univ. Texas Bull.
1932, pp. 19-20.
'These facts were discovered by Dr. J. A. Udden, who has kindly permitted their
use here.
4SelIards: On the Underground Position of the Ellenburger Formation in North
Central Texas, Univ. Texas Bull. 1849, 1920.
Weno and Pawpaw Formations
15
and is increasing southeastward at the rate of about 8 feet per mile. (Hill).
Likewise the Paluxy entirely disappears to the south. There are in addition
two complicating circumstances, which affect the thickness and lithology,
general regional thickening and depositional facies. The Fredericksburg
division increases steadily in thickness from the Red River to beyond the
Rio Grande. Its marl and marly limestone facies persist at most levels to
APPROXIMATE THICKNESS OF THE COMANCHEAN FORMATIONS OF
NORTH TEXAS, IN FEET
t
FORMATION
»
§ Bryan and Marshall
? Counties, Oklahoma
| Grayson County, Texas
^
§ Cooke County
•+
x
=> Denton County
o Tarrant County
Parker County
D
= Johnson County
5
P
5 Hill County
-f
Buda
Grayson
50
50t
60
82
80
100
Mainstreet ....
5
10 15
40
50
50
50
35J
Pawpaw
56
50
45
27-40
12-27
9 18
5
Weno
114
125
110 '
ro-ioo
62
40
25
Denton
25
25
25
25
25
20-26
5
Fort Worth
30
30
30
30
32
30
25 27
25
Duck Creek marl . . .
Duck Creek limestone
Kiamitia
40
100
130
60
130
61
30J
50J
40
30{
50t
30-40
22
45
27-31
201
40 f
30
20
40
18
50
19
Goodland
16
12-20
19
117
Edwards
20
35
40
Comanche Peak ....
120
105
150
Walnut
8
(5)
5-15
]
125-150
150
100
150
Paluxy
150
150
90
150
Glenrose
?
470
100-300
400 -500
Basement Sand
WASHITA(exclu-
s i v e Woodbine . .
FREDERICKS-
BURG
250
550J
25?
250
541J
50
200J
430
25?
200?
394
150J
374
242
150J
120
290
150
338
330
164f
350
TRINITY
?
200?
770J
650
COMANCHEAN...
825
841
655
1386
^Approximate thickness.
16 University of Texas Bulletin
•
the region between the Brazos and the Colorado Rivers. South and west of
this region the Rudistid facies invades the Fredericksburg division, begin-
ning with the level representing the top of the Edwards limestone (see page
24). The Rudistid facies is characterized by considerable thickness of
indurated massive limestone, so that southward as this facies vertically
invades the stratigraphic column the invaded formations thicken, Rough
estimates of the thickness of this division are: Red River (Denison, 50
feet ; Goodland, Oklahoma, 25 feet) ; Trinity River (Fort Worth), 242 feet;
Colorado River (Austin), 350 feet. And for the Washita division: Den-
ison, 541 feet; Fort Worth, 374 feet; Austin, 220 feet.
In the following table of approximate thicknesses it should be noted that
the basal Comanchean deposits are transgressive northwards in such a
manner that we do not know with certainty what part if any of the Base-
ment Sands of Cooke, Grayson and Denton Counties is of Trinity age. The
lowest determined Comanchean fossils in this area indicate the level of
Exogyra texana and its varieties of Walnut age. In the Duck Creek forma-
tion of the table the "marl" is taken to be the portion above the Mineralized
Ledge1 (Stratum 17) of the Fort Worth region, i. e., above the horizon of
abundance of Scaphites worthensis.
LITHOLOGICAL CHANGES
The lithology of the Washita division is diverse and each formation
must be considered separately. However, it is generally true in North-
Central Texas that the formations decrease in thickness southwards to
the Brazos-Colorado divide south of Waco, Texas ; these changes in thick-
ness and lithology may be considered as a unit, and are related to the
depositional conditions in the large North-Central Texas trough already re-
ferred to. Crossing the Brazos-Colorado Divide in which the thinned Penn-
sylvanian and Ellenburger and pre-Cambrian floor are structurally high,
there is in the Cretaceous another set of thickness changes which for cer-
tain formations, notably the Buda, amount to a regional increment in
thickness as far south as the turning point of the Washita outcrops in
Bexar County. Westward from this point there appears a little known set
of changes in thickness and lithology of these formations. In West Texas
again, the northern, near-shore facies (Cerro de Muleros, Finlay Moun-
tains, Kent, Sierra Blanca) passes quickly into the southern, massive
limestone, in part rudistid facies (Shafter, Terlingua, Fort Stockton, Shef-
field) and the Texas and Pacific Railway is approximately the boundary
line between these two facies. The transition zone from the Edwards
1Winton and Adkins: The Geology of Tarrant County, Univ. Texas Bull. 1931
pp. 42-43.
Weno and Pawpaw Formations 17
limestone level passes between Fort Stockton and Sheffield and eastward to
a point near Pecos, thence some distance north of Coke and Runnels coun-
ties, north of the Central Mineral Region, and approximately to the north-
ern border of Hood County, near Comanche Peak. Here the Edwards out-
crop disappears eastward under the later formations. An extended study
of the rudistid facies will be necessary to define this boundary line pre-
cisely ; but it is cited here as an illustration of the type of lithological vari-
ations seen within the extent of the Texas Comanchean outcrops. For the
other Washita formations likewise, much field work will be necessary to
map even approximately their different lithological facies ; accordingly the
following summary of these formations is brief and condensed.
GRAYSON FORMATION
Sandstone facie*:
Unknown.
Clay facie*:
Upper half of the Del Rio Clay (approximately the Gryphea mucronata
zone, south of the Brazos River). The middle member of the Grayson
is a clay as far north as Denton County, Texas.
Marl facie*:
Near Bennington, Durant and Bokchito, Oklahoma, Denison, Fink,
Gainesville, Denton, Fort Worth, and Burleson, Texas. This is the pre-
vailing facies along the outcrop. The eastermost exposure in Central
Texas is east of Roanoke, Texas, where the few, insignificant limy seams
seen in the Fort Worth region are represented by eleven conspicuous
limestone strata. There is little doubt that this formation grows rap-
idly more calcareous eastward and southeastward, and that its limestone
facies lies in this direction from the outcrop in North-Central Texas and
not far from the outcrop. Passing down the Red River valley, however,
this does not hold, for the formation is marly in the Tishomingo quadrangle
and near Bennington, Oklahoma, where it has essentially the same lithology
and fossils as in Tarrant County, Texas.
WEST TEXAS
In the Cerro de Muleros section, Bose's subdivision 81 consisting of
yellow marls containing Schloenbachia sp., Pecten subalpinus (Bose),
Exogyra whitneyi Bose,2 Hemiaster calvini Clark, Protocardia texana
(Conrad), and Enallaster bravoensis Bose, is Grayson. It overlies the
Mainstreet formation, here a sandstone, and underlies subdivision 9, a
'Bose: Inst. Geol. Mex. Bol. 25, p. 27-28.
2B6se: Univ. Texas Bull. 1902, p. 10.
18 University of Texas Bulletin
limestone which may be either Grayson or Buda, probably the latter ; this
underlies the Woodbine (Dakota) sandstone. The Kent section contains
equivalents of Weno and Pawpaw in division 3 of Durable and Cummins1
section, which however does not permit of more precise definition.
A north-south line drawn two miles east of Roanoke, Denton County,
therefore delimits the marl facies of the Grayson from the transitional beds
to the limestone facies, since east of this line the Grayson becomes calca-
reous. This line however probably turns east since on going down the Red
River valley it leaves the marl facies of the Grayson to the north at seen at
Denison, Bennington and numerous other places in Southern Oklahoma.
What relations exist east and south of these points depends on well records
not yet investigated. South of the Brazos River near Waco there is at the
Grayson outcrop a transitional zone to the southern clay facies (zone of
Gryphea mucronata, upper half of the Del Rio Clay) which continues west-
ward to the El Paso region. The sand facies is unknown but is to be ex-
pected in the removed areas of North Central Texas, in the isolated Upper
Washita remnants of the Panhandle not yet investigated, and in the Tu-
cumcari region.
Limestone facies:
The limestone facies, on the other hand, lying southwards in Sonora and
Chihuahua is still unidentified in Texas, except at one point, the Mariscal
Mountains, at the south tip of the Big Bend region.2
MAINSTREET
Sand facie*:
At Cerro de Muleros, near El Paso, Texas ; apparently near Santa Rosa,
New Mexico (Dr. Bb'se) .
Clay facies (Del Dio Clay, in part) : The Del Rio Clay is poorly known,
and therefore its correlation is tentative. It is equivalent to the Grayson
and the upper part of the Mainstreet, and contains the following fossil
levels :
(1) Nodosaria texana Conrad. A zone of abundance above that of
Exogyra cartledgei Bose3 in the upper 30 feet of the formation, which at
Shafter reaches a thickness of 190 feet. Below this zone of abundance
Nodosaria is scattering.
(2) Gryphea mucronata Gabb. Upper half of the Del Rio Clay.
(3) Exogyra anetina Roemer. Rare near the middle of the clay in
tumble and Cummins: Amer. Geol., xii, 1893, 309.
2Udden, Baker and Bose: Univ. Texas Bull. 44, 1919, p. 76.
3B6se, Univ, Texas Bull, 1902,
Weno and Pawpaw Formations 19
West Texas, abundant lower; in Central Texas (South Bosque, Round
Rock, Austin) it is abundant in the basal half of the formation but rare or
wanting above. It also occurs in the top of the Georgetown limestone at
Austin.
(4) Turrilites brazoensis Roemer occurs in the lowest five feet of the
Del Rio Clay at South Bosque and at Austin ; its main zone of abundance is
in the top of the underlying Georgetown limestone.
Zones (1) and (2) are Grayson; zones (3) and (4) are Mainstreet; or
briefly the upper part containing Gryphea mucronata is Grayson, and the
lower part containing Exogyra arietina is Mainstreet. The Mainstreet
equivalents locally have sandy levels in Central Texas, as for instance at
the top of the Georgetown limestone at South Bosque and in the E. arietina
slabs at Austin. Westward from the turning point of its outcrop in Bexar
County the Del Rio becomes sandier and more flaggy and contains sandy
slabs with Nodosaria and other fossils. At the south end of the Quitman
Mountains the Del Rio is transitional, showing a mixture of sand and clay
facies, and at Cerro de Muleros the Mainstreet, represented by Bose's sub-
division 7 is sandstone. North of the turning point the typical Central
Texas section continues to the Brazos, where the Del Rio differentiates into
two portions by the intercalation of limestone strata basally; this basal
part becomes upper Mainstreet and the upper marlier part becomes Gray-
son. The lower Mainstreet however continues as a limestone into Central
and West Texas.
Marl facie*:
The upper Mainstreet formation in McLennan County is transitional
from clay to marl, and at South Bosque is rather calcareous. North of the
Brazos this calcareous marl contains limy seams which become more prom-
inent and take on the interbedded appearance of the Mainstreet limestone
of North Texas.
Limestone facie*:
The typically developed Mainstreet limestone between the Brazos and
the Red Rivers shows this lithological facies. There is considerable inter-
bedded marl as far north as Gainesville. Eastward from Gainesville, down
the Red River Valley, at Cedar Mills, Denison, Bennington, Bokchito and
near Hugo, the marl is more reduced in amount, and the formation consists
of compact, slightly marly, massive shell breccia or indurated limestone
with typical Mainstreet fossils.
20 University of Texas Bulletin
PAWPAW FORMATION
The Pawpaw formation shows along its north-south outcrop an almost
idealized sequence of marine facies.
Sand facies:
Red River Valley, as far south as the southern border of Cooke County,
Texas.
Clay faciet:
Denton, Tarrant and Johnson counties, Texas, to near Riovista.
Marl faciei:
Johnson and Hill counties, Texas.
Limestone facies:
The equivalents of the Pawpaw south of the Brazos are questionable.
If it is represented in this region, it is the upper part of the Georgetown
limestone. (See page 11.)
In West Texas its exact equivalent is unknown. At Cerro de Muleros
however a distinct Weno and possibly Pawpaw fauna are present in Bose's
subdivision 6, but not enough distinctive Pawpaw species are recorded to
decide how much of this subdivision represents it. A hiatus at the base
and at the top of the Pawpaw has been noted by Stephenson,1 near the Red
River, but it is unlikely that this accounts for any great thickness of Wash-
ita sediments.
WENO FORMATION
Sand facies:
There is sand in the upper half of the Weno, in the Red River Valley,
Denison, Cedar Mills, Gainesville, Texas. In the lower half of the Weno :
unknown. At Tucumcari, New Mexico, Dr. Bb'se found a sandstone, prob-
ably Weno-Pawpaw, containing Ostrea quadriplicata Shumard, TurriteUa
sp., Protocardia multistriata (Shumard), Protocardia sp. aff. texana
(Conrad), Gryphea dilatata Marcou2 and other fossils.
Clay (shale) facies:
Red River Valley, Gainesville and Denison, Texas. Contains a few thin
ironstone seams; southward and to a less extent eastward this facies be-
comes marly and is intercalated with thin limestone seams.
Marl facies:
Denton, Tarrant, Johnson and Hill counties, Texas. The upper half
of the Weno is limy at places (as Fort Worth) where the lower half is
marly. The formation is prevailingly of limestone throughout, south
'Stephenson: U. S. G. S., Prof. Paper 120-H, p. 143.
2Marcou: Geology of North America, plate IV, figures 1, la, 3, 1842.
Weno and Pawpaw Formations 21
of the Brazos River. In West Texas at Cerro de Muleros, the Weno is rep-
sented in Bose's subdivision 6, which consists of marls, sandstone and lime-
stone. This series is therefore composite and transitional, like the Weno
at Gainesville and Denison, and contains many identical fossils.
Limestone facies:
Portion of the Georgetown limestone near top, south of the Brazos. An
indurated, massive limestone facies is unknown but probably lies to the
east and south of the outcrop in Central Texas.
DENTON FORMATION
Sand facie*:
Unknown.
Clay facies:
From Blue Mound, near Haslet, Tarrant County, Texas, northward to
Denison. Contains pyrite and crustacean fauna.
Marl facie*:
In North-Central Texas along the outcrop the marl facies appears below
Blue Mound, just north of Fort Worth and continues southward. In
southern Oklahoma, the Red River Valley and Central Texas north of the
Brazos, this formation is a clay, slightly arenaceous at the base and capped
by shell conglomerate. This conglomerate is much more conspicuous at
the Red River than at Fort Worth and southward, where it has largely
disappeared, leaving a very shelly marl. South of the Brazos River, near
Waco, there is a transitional zone between the marl and the limestone
facies.
At Cerro de Muleros a portion of subdivision 5 is a gray marl containing
great numbers of Gryphea washitaensis Hill, and represents the Denton.
Limestone facie*:
The portion of the Georgetown limestone which represents the Denton
formation is a consolidated shelly limestone with very little calcareous
cementing material, and usually massive without marl interbedding. It
extends from a point near Waco southwards to the turning point of the
Comanchean outcrops in Bexar County and thence westward to beyond
the Pecos River. In the El Paso region, however, the equivalent to the
Denton belongs to the northern (littoral-bathyal) facies and is marly as
in North Texas.
FORT WORTH FORMATION
This formation is calcareous over all of North and Central Texas but is
somewhat marly in the Red River valley and is prevailingly marly near El
22 University of Texas Bulletin
Paso. A line connecting these two areas will give very roughly the boun-
dary between the marl and lime areas.
Sand faciet:
Unknown.
Clay facie*:
Unknown.
Marl facie*:
Cerro de Muleros, near El Paso, gray to bluish marls ; Denison and east-
wards, marly limestone and marly interbedding.
Limestone facie*:
South of the Red River and throughout North and Central Texas at the
outcrop. The middle portion of the Georgetown limestone represents this
facies. A deeper sea subphase found in southern Trans-Pecos Texas con-
sists of hard, crystalline, sparsely fossiliferous, relatively pure, fine grained
lithographic limestone, which composes most of the Georgetown and Buda.
This is the purest and probably the deepest sea deposition known for this
formation.
DUCK CREEK (Upper)
Sand facies:
Unknown.
Marl facie*: •
This group of strata is prevailingly a calcareous marl and contains the
least limestone at Gainesville. At Fort Worth it has only slightly more
lime than at Gainesville, while at Denison and at Caddo, Oklahoma, it is
distinctly more limy. The change from marliness to liminess therefore
appears to be in this region at least largely an east- west change. The
Duck Creek marl thickens to the northwest, being thickest near Denison
and thicker in the Tishomingo than in the Atoka area.
Limestone facie*:
South of the Brazos-Colorado River divide, the Duck Creek marl is im-
bedded in the base of the Georgetown limestone, where it is a marly im-
pure limestone.
The situation in West Texas is unknown.
DUCK CREEK (Lower)
Sand facies:
Unknown. There are some bituminous sandy layers in the Duck Creek
in Cooke County, Texas, but these appear to be local.
Shale (clay) facie*:
Seen at the type locality, three miles north of Denison, Texas. This
shale is somewhat calcareous and is transitional to a marl.
Weno and Pawpaw Formations 23
Marl facie* :
This facies invades the limestone series at Gainesville, Texas, where
all of the lower Duck Creek except the basal ten feet is prevailingly marly.
Probably the removed portion of the Duck Creek west and north of the
outcrop was prevailingly marly.
Limestone facie*:
Extends from Denton County southward to the turning point of the
Comanchean outcrop in Bexar County, and thence westward to the Trans-
Pecos region. The group of strata is composite and at a given point is
more marly above than below. For instance, at Denison the Hamites and
Desmoceras zones are prevailingly limy marl with some blue shale, and at
Denison the zone of Desmoceras brazoense is marly at the top; at Fort
Worth the section is limestone to the top of the Schloenbachia trinodosa
horizon and limy even above this ; while below the Brazos the whole lower
Duck Creek section becomes limy.
South of the Brazos the Duck Creek formation lies at the base of the
Georgetown limestone where it is a chalky white indurated rather un-
fossiliferous limestone, differing considerably in appearance at Austin
and at Georgetown, Texas; while west of the southern turning point of
the outcrop it becomes a hard, crystalline, consolidated, sparsely fossilifer-
ous limestone. At Cerro de Muleros near El Paso, on the contrary, the
northern littoral facies is present as at Gainesville and Denison and this
level is represented by a series of clay, marl and limestone, which repre-
sents a transitional facies. Vraconian faunae from Chihuahua and Zaca-
tecas (p. 60) represent in part this stratigraphic level.
KIAMITIA FORMATION
Sand facie*:
Unknown.
Clay (abate) facie*:
From near Primrose, southwestern Tarrant County, south througn
Johnson County to beyond the Brazos. This formation at Blum, Hill
County, is a yellowish clay 19 feet thick. This facies contains a con-
spicuous limonite fauna, Schloenbachia, Area, small gastropods and pelecy-
pods and other fossils.
Marl facie*:
Southern Tarrant County to between Gainesville and Fink. The forma-
tion is increasing in thickness northwards and as the clay facies disap-
pears, flag layers enter first as limestone in thin sheets and farther north
as shell conglomerate sheets. The bulk of the formation is marl, and the
limonite fauna has largely disappeared.
24 University of Texas Bulletin
Lime facies (conglomerate):
Fink, Grayson County, Texas, to east of Hugo, Oklahoma. Coincident-
ally on passing eastwards and northwards from the marl facies the scat-
tered shells in the formation become consolidated into conglomeratic sheets
with shelly marl between, and these predominate at Gainesville and Deni-
son. Turning east down the Red River Valley the thickness of the Kia-
mitia and the amount of this conglomerate greatly increase. Near Hugo,
Oklahoma, the Kiamitia shell conglomerate is about 150 feet thick and is
extensively used for crushed rock. This formation is a shallow water
oyster bed deposit of mixed Fredericksburg and Washita fossils, mainly
the former.
The formation disappears at the Brazos-Colorado uplift, and in West
Texas its relations are unknown.
EDWARDS FORMATION
The Fredericksburg Division also must be considered sectionally, since
its various parts behave differently as to their changes of thickness and
lithology.
Sand facies:
Unknown.
Clay facies:
Unknown.
Marl facies:
Unknown. Bose's subdivision 3 at Cerro de Muleros contains some
marl, but this subdivision is not positively known to be Edwards. Through-
out the Red River region and North-Central Texas, the top of the Good-
land, which is thought to correspond to the Edwards, is a non-marly lime-
stone, usually massive and sometimes crystalline. North of Sheffield and
Fort Stockton, the Fredericksburg is stated to be prevailingly marly.
Limestone facies:
This is known from Fort Worth south to the turning point of the out-
crop in Bexar County, and thence west to El Paso. The Red River ex-
tension of this level is not identifiable with certainty because it is not
clear whether the 12-20 feet of white limestone at the top of the Fredericks-
burg division as seen at Denison or north of Goodland, Oklahoma, repre-
sents only the Edwards or also in part still lower Fredericksburg. The
Edwards is less than 10 feet thick at Fort Worth; it is 33 feet thick at
Comanche Peak, and southwards thickens rapidly.
Rudistid facies:
The Rudistids invaded Texas most widely in upper Fredericksburg time,
when they were scattered as far north as Fort Worth ; however, they are
very rare and inconspicuous north of the Brazos, in Central Texas. In
Weno and Pawpaw Formations 25
West Texas they are reported as far north as Bailey County, and they
are common in Coke and Runnels counties. In Trans-Pecos Texas, the
Texas and Pacific Railway roughly divides the southern rudistid facies
of the Edwards from the northern littoral facies. The rudistids are
rare or wanting at Cerro de Muleros, Kent, Sierra Blanca and the Finlay
Mountains ; and present at points between these and the Rio Grande. Gabb1
describes from the Sierra de las Conchas near Arivechi, Sonora, fossils
which if correctly identified include among diverse stratigraphic levels
that of the Edwards limestone ; the facies represented is unknown to me.
Felix and Lenk'- also record the great extent of the Fredericksburg reef
facies in Mexico.
WENO AND PAWPAW FORMATIONS
The influence of the underlying syncline on the deposition of these two
upper Washita formations is small, due to their small thickness. However,
they show an appreciable syncline in the Fort Worth region, and a con-
spicuous thinning southward.
Since the maximum rate of change of thickness, like the maximum
change in lithology, may not coincide in direction with the outcrop, the
formation along the outcrop will in general show only a greater or less
north-south or an east-west component of change in thickness or lithology
and the maximum change will be in a direction lying at an angle to the
outcrop.
THICKNESS CHANGES
North-South Changes
This is true of the north-south outcrop of the two formations, which
does not exactly coincide with the direction of greatest thickness change.
The Weno and Pawpaw strata outcrop in a line passing about a mile east
of Gainesville, Cooke County, and thence nearly south to near Denton;
thereafter the boundary between the two formations runs near Fort Worth,
west of Cleburne, Riovista and Blum.
The outcrop thus from the Red River to the Brazos has a general trend
of east of north, while the direction of greatest thickness change is slightly
east of north. (See figure 3).
'Gabb: Pal. Cal., vol. 2, p. 257 ff.
2Pelix and Lenk: Beitr. z. Geol. u. Pal. d. Rep. Mex., II, p. 28.
26 University of Texas Bulletin
East-West Changes (North Texas and Oklahoma)
In the whole Red River region these two formations at their outcrops
maintain an almost uniform thickness, but they are slightly thicker east-
ward as far as Choctaw County, Oklahoma. Their behavior east of this
point is unknown to me.
TABLE OF APPROXIMATE THICKNESS OF WENO AND PAWPAW
FORMATIONS
Weno Paw-
Locality Lower Upper Total paw
Denison 45 80 125 60
Gainesville 40 70 110 44.8
Blue Mound (Haslet) 27.3
Fort Worth 12.7 49.6 62.3 24.6
Riovista '. 10 25 35 5.0
LITHOLOGICAL CHANGES
The Weno and Pawpaw formations are marked by striking lithological
changes which produce along their outcrops localized lithological regions
each with a characteristic fauna. The Pawpaw formation, and to a less
extent the Weno, passes from north to south along its outcrop through a
"typical" series of lithological fades— sand-clay-marl-limestone, which
aside from various complicating factors of deposition is usually taken to
represent a progressive series of marine facies from near-shore .to off-
shore conditions. Likewise the problem of localized faunales is vividly
impressed upon one by the situation in the Pawpaw clay (as also in the
Weno), where within a few miles one fauna largely disappears and an
equally rich and varied, but different one occupies its stratigraphic posi-
tion. For example the Gainesville-Denison fauna (Nacreous, Area), the
Fort Worth fauna (Turrilites, Engonoceras, Hamites, Scaphites) and the
Riovista fauna (Flickia, echinoids) of the Pawpaw formation represent
three different marine facies. The narrow ribbon-like outcrop of these
formations in North Central Texas and Southern Oklahoma gives only a
limited opportunity for the study of these different marine phases, but the
following regional differences in the sediments of these formations are ap-
parent.
Weno and Pawpaw Formations
PAWPAW FORMATION
Nature of Material Locality of Outcrop
27
(a) Semi-consolidated sandstone and
ironstone
Choctaw county, Oklahoma
Marshall county, Oklahoma
Bryan county, Oklahoma
Love county, Oklahoma
Grayson county, Texas
Cooke county, Texas
Faciea
of Marine
Deposition
(b) Clay with sandy layers f Denton county
| Tarrant county
(c) Marl with limy layers. . . f Johnson county
{ Hill county
(d) Limestone South of Brazos River
Neritic
Bathyal
Deeper Sea
(a)
(b)
(c)
UPPER WENO
stone | Cooke county Neritic
Marl with lime layers Denton county Bathyal
Limestone Tarrant county and south wardDeeper Sea
(in part Zoogenic)
LOWER WENO
(a) Shale with sand layers Red River region Neritic
(b) Marl and limestone layers Cooke county to Brazos RiverBathyal
(c) Limestone South of Brazos River Deeper Sea
PAWPAW FORMATION
Eastward from the turning point of the Comanchean outcrops in the
Red River uplifted area near Orlena, Cooke County, Texas, the Pawpaw is
a ferruginous sandstone or an unconsolidated sand. This outcrop runs
down the Red River valley in a direction a little south of east, lying in
Cooke and Grayson Counties, Texas, and in Love, Marshall, Bryan, and
Choctaw Counties, Oklahoma.
Sandstone Facies
(a) (Semi-consolidated Sandstone and Ironstone)
In general, the Pawpaw formation is prevailingly sandy and iron bear-
ing at its outcrops north and east of the south border of Cooke County,
Texas.
28 University of Texas Bulletin
Near Gainesville, the formation is a series of thickbedded, hard, ferru-
ginous sandstones with interbedded, laminated impregnated sandy layers
and semi-consolidated iron-impregnated sand. The layers are locally a
shell conglomerate containing great quantities of casts of Area, Turritella
and other bivalves and gastropods. The basal layers are characterized by
an abundant pyrite fauna. Turrilites, Scaphites, Hamites and echinoids
are rare or absent. This type of lithology continues around the turning
point of the Comanchean formations south of Orlena to a point near Potts-
boro; and at Denison the Pawpaw formation is almost entirely a coarse
consolidated brownish-red sand with few fossils. At Durant the formation
is similar to the Denison exposures. Eastward through Bennington and
Bokchito the sandy phase continues, and is included in the Bokchito for-
mation of Taff.
SECTION OF SUGAR LOAF MOUNTAIN, BRYAN COUNTY, OKLA-HOMA
Section 22, R. 12 E., T. 5 S. (furnished by W. M. Winton)
MAINSTREET:
Limestone, iron stained, old cap of hill, practically removed by weathering.
Feet
PAWPAW:
Massive yellow red sandstone, soft in fresh exposures, indurated where long
exposed ; no fossils seen 5.0
Soft limonitic sand ; no fossils seen 30 . 0
Ironstone ledge composed of fossils (Area sp., Ostrea quadriplicata, small
ammonites, gastropods, etc., a typical Pawpaw fauna) 0.5
Red sand, cross bedded and containing lenticular hard masses of sandstone 10.0
Ironstone ledge composed of fossils (Area sp., Ostrea quadriplicata, am-
monites, Nodosaria, etc., a typical Pawpaw fauna) 0.8
Red sand 10.0
WENO:
Yellowish hard limestone with typical Weno fossils 0.8
Soft marl ; no fossils seen 0.3
Very hard massive limestone, pinkish in color. Large numbers of fossils
having same hardness as matrix and giving uniform fracture. Ledge
forms conspicuous topographic break traceable for miles. Schloenbachia
sp. M., and other typical Weno fossils 1.9
Soft marl 15.0
Limestone ledge sandy; no fossils seen 1.0
Soft marl with a few thin limestone ledges, each less than 0.5 feet thick 95.0
DENTON:
Conglomerate of Gryphea washitaensis, Ostrea carinata, and other Denton
fossils. Typical Denton marl ("Caddo" limestone of Taff, top). Ex-
posed, about < 2.0
Weno and Pawpaw Formations 29
In the creek, one-fourth mile west of the mountain, the contact between the Duck
Creek marl and the Fort Worth limestone is exposed as at Caddo, Oklahoma.
In the second cut 1V£ miles north of Hugo, Oklahoma, there is 10 inches
of shell conglomerate containing abundant juvenile and adult Ostrea
quadriplicata Shumard, Gryphea washitaensis Hill, Plicatula sp., Pecten
subalpinus (Bose), abundant Leiocidaris spines, Corbula littoralis Adkins,
and other typical upper Weno fossils as found at Gainesville and Denison.
This represents part of the Quarry limestone group. Above it is an iron-
stone ledge, 4 inches thick, which is red-stained and conglomeratic and re-
sembles the basal Pawpaw as seen at Gainesville.
Along the St. Louis and San Francisco Railway track between Benning-
ton and Bokchito, Oklahoma, the upper Washita section, Woodbine to
Weno, is seen to advantage. The Grayson marl with an estimated thick-
ness of 50 feet is well developed with its characteristic fossils.1
The Mainstreet limestone is seen in roadside cuts one mile northwest of
Bennington, in the caprock of Sugarloaf Mountain, six miles north of Ben-
nington, in the bed of Sulphur Creek, where it forms an extensive pave-
ment limestone, and in the railroad cuts nearby, particularly in the long
cut running west down to Bokchito Creek, which has it well exposed.
Everywhere it is underlain by the brown consolidated Pawpaw sandstone.
The nature of the Pawpaw and Weno outcrops in this region is seen from
the following section.
SECTION OF CUT NEAR SULPHUR CREEK, ON THE ST. LOUIS AND SAN
FRANCISCO RAILWAY, TWO MILES WEST OF BENNINGTON, OKLAHOMA
MAINSTREET: Feet
Brown limestone with Turrilites brazoensis, Pecten subalpinus, Exogyra sp.
(large), and ammonites. The top of the exposure is an Exogyra
arietina conglomerate. Exposed 2
Brown-blue limestone with irregular sandy inclusions 1
Yellow limestone containing Kingena wacoensis, Ostrea marcoui, and Pecten
subalpinus 1 . B
'Taff (U. S. G. S. Geologic Atlas of the United States, Atoka Folio, No. 79) has
overlooked the Grayson marl, which in this quadrangle is typically developed as at
Denison. It may be seen near the Woodbine ("Silo") sandstone knob mapped by Tafl
one mile northwest of Bennington, Oklahoma, where it overlies typical Mainstreet
limestone containing Turrilites brazoensis Roemer, Exogyra arietina Roemer and othei
distinctive fossils, and contains Gryphea mucronata Gabb, Gryphea, sp. (truncate)
Pecten subalpimts (Bose), Plicatula sp., Ostrea sp. aff. subovafa. Shumard, and
Kngonoceras sp. This locality is mentioned by Taff, ibid., p. 6. It also forms the
overburden in the Mainstreet quarry one mile north of Durant, Oklahoma, where it
is very fossiliferous.
30 University of Texas Bulletin
PAWPAW:
Consolidated brown sandstone, no fossils seen 5
Unconsolidated sand, iron stained 10
Blue jointed clay with scattered Gryphea 10
!<ed-brown sandstone — calcareous in part — with nacreous and ironstone fos-
sils: Area, Nucula sp., Corbula sp., Cerithium, Turritella, Anchura,
like the Gainesville and Denison nacreous fauna 1
Marl, containing ironstone seams, no fossils seen 10
The cut east of the Bokchito Creek bridge shows the foregoing section
much better exposed. Pawpaw exposures were also noted near Durant,
Oklahoma. North of the railroad, 11/2 miles east of Bennington, Oklahoma,
about 50 feet of massive brown sandstone was noted underlying the Main-
street limestone at the top of the hill. This sandstone contains limy layers
bearing Ostrea quadriplicata, 0. subovata(l), marcoui, Trigonia sp., Gry-
phea sp., and Pecten sp. (large). Taff gives the following section for his
Bokchito formation in the Atoka and Tishomingo quadrangles1 :
SECTION OP THE BOKCHITO FORMATION IN THE ATOKA AND TISHOMINGC
(OKLAHOMA) QUADRANGLES
J. A. Taff, 1902-1903
Feet
4. Sandy and clay shales, and locally friable, cross bedded sandstone. In the
clay and in some of the iron and lime concretions, shells are preserved
with original nacre 50
3. Hard, semi-crystalline, bluish, oyster shell limestone, weathering yellowish
and projecting as ledges separated by friable shales 10-20
- 2. Friable sandstone beds, locally cross bedded, alternating with and including
deposits of sandy clay 20-3C
1. Sandy clay shale, with ferruginous limestone segregations and ironstone
nodules 90
170-190
This thickness is given as 140 feet in the texts and the Columnar Section sheets of
both folios.
The upper member (4) of this section is probably Pawpaw. Sheets of
nacreous shells in the Pawpaw have been noted in Grayson County. The
other three members are Weno.
The Pawpaw formation is exposed in the hilltops east of Denison and
iTaff: U. S. G. S., Geologic Atlas of the United States, Atoka Folio No. 79, 1902.
p. 6; and, Tishomingo Folio, No. 98, 1903, p. 6.
Weno and Pawpaw Formations 31
may be seen in cuts on East Main Street, where it is a cross-bedded rather
consolidated, brick red sandstone. No fossils were seen at this locality.
The formation is stated by Stephenson1 to be 50 or more feet thick near
Denison. The Pawpaw is poorly exposed north of a west branch of Little
Mineral Creek just south of Fink, where it is steeply tilted. On the Red
River about 2 miles northwest of Cedar Mills, Grayson County, there is a
long cliff dipping west (5°) which exposes near the top about 40 feet of
loose sand only partially consolidated, which is probably Pawpaw.
SECTION OF BLUFF OF RED RIVER TWO MILES NORTHWEST OF CEDAR
MILLS, GRAYSON COUNTY, TEXAS
MAINSTREET: Feet
White limestone with Ostrea quadriplicata, Turrilites brazoensis, Kingena,
Exogyra arietina, Pecten subalpinus, Enallaster sp. aff. texanus. Seen
in ravine above east end of river bluff near road 10
PAWPAW:
Sandstone with thin ferruginous layers 40
Blue marl with clay and sand seams and nacreous fossils: Engonoceras,
Corbula, Nucula, Ostrea quadriplicata, Pecten subalpinus 30
QUARRY LIMESTONE (?):
Massive grayish semi-crystalline limestone • 2
WENO:
Blue marl with nacreous fossils 40
The roadside cuts 2i/2 miles east of Gainesville, Cooke County, inconsec-
utive sections of the Pawpaw are seen. The interval from the top of the
Quarry group to the base of the Mainstreet limestone is not less than 45
feet. The base of the Pawpaw overlying the Quarry limestone is seen in a
cut of the Missouri, Kansas and Texas railway (Wichita Falls branch) at
the north end of the brickyards pit 1% miles southeast of Gainesville.
This exposes about 8 inches of an irregularly deposited reddish ferrugin-
ous shell conglomerate largely of Ostrea quadriplicata — cemented into the
pitted surface of the Quarry limestone. The same level is exposed near
the water tank on the southwest rim of the pit. In roadside cuts •% mile
southeast of this locality about 45 feet of Pawpaw may be seen poorly ex-
posed ; it consists of thin layers of ferruginous dark red brown sandstone
which, locally at least, consists of cemented masses of ironstone fossil casts :
Area, Protocardia, Nucula, Corbula, Turritella and rare Ostrea quadripli-
cata and Gryphea. These ironstone layers are interbedded with brown to
iStephenson, U. S. G. S., Prof. Paper 120-H, p. 142.
32 University of Texas Bulletin
yellow, softer, ferruginous, very arenaceous clay. Their ironstone seams
do not exceed 6 inches in thickness and locally are highly indurated.
SECTION OF THE PAWPAW FORMATION IN ROADSIDE CUTS TWO ANE
ONE-HALF MILES SOUTHEAST OF GAINESVILLE, TEXAS
^Section furnished by W. M. Winton
MAINSTREET: Feet
White massive limestone with characteristic Mainstreet fossils. Exposed ... 6
PAWPAW:
Alternating red ironstone and ferruginous sandy clay layers. About 16
compact ironstone layers each 3 to 4 inches thick, alternating with clay
layers each about one foot thick. The ironstone layers are similar from
bottom to top and the basal 10 feet is more fossiliferous than the upper
portion. The ironstone layers contain: Remondia sp., Trigonia sp.,
Area sp., Engonoceras sp., Nucula sp., Corbula sp., and other nacreous
and ironstone fossils 21 . 5
Brown sandstone flag layer 0.5
Red ironstone layer with Nodosaria texana 0 . £
Brown clay 5 . C
Red ironstone with Area sp., Ostrea quadriplicata O.B
Brown clay, sparsely fossiliferous : Area, gastropods 15 . C
Red calcareous sandstone: Ostrea quadriplicata 2.C
This is underlain 'by the Quarry Limestone group (see page 36). The
thick semi-consolidated sand seen in Grayson County is absent. The Paw-
paw outcrop which has turned nearly south at the turning point near Or-
lena, makes a narrow north-south strip from Gainesville to the southern
border of Tarrant County. The ironstone facies does not persist past
the Trinity River, since interstratified clay lenses here largely make up the
formation ; as far south as Fort Worth there are large amounts of weath-
ered ironstone fragments in the surface debris of the Pawpaw.1
Clay Facie*
This facies of the Pawpaw formation is best developed in the Fort Worth
region. From Cooke County southward to the Brazos the Pawpaw is rap-
idly thinning, as previously described. At the same time, passing south-
ward through Denton and Tarrant Counties the clay facies is encountered,
and in the region of the Brazos the marl facies appears. The clay facies
grades into each of the other two facies, so that the transitions are gradual.
This gradation occurs through the invasion of one facies by seams of the
other kind of material.
'Winton and Adkins: Univ. Texas Bull. 1931, p. 67.
Weno and Pawpaw Formation? 33
The transitional zone from the ironstone to the clay facies occurs in Den-
ton and northern Tarrant Counties. As far south as the Trinity River con-
siderable amounts of ironstone fragments occur in the Pawpaw exposures ;
these are the residue of numerous thin ironstone ledges similar to those of
the Red River area but sparsely fossiliferous, which are scattered rather
evenly throughout the formation. The interbedding material is an arena-
ceous clay. South of the Trinity the section is prevailingly clay but has
thin ironstone, limestone and sand seams.
SECTION OF THE PAWPAW FORMATION AT BLUE MOUND ONE AND ONE-
HALF MILES SOUTH OF HASLET, TARRANT COUNTY, TEXAS
MAINSTREET: Feet
White chalky limestone, exposed 4
PAWPAW:
Brown to yellow, sparsely fossiliferous clay, with thin ironstone seams and
scattered sand lenses 23
Sandstone flag layer 0.3
Brownish yellow impure clay 4
Thickness of Pawpaw 27 . 3
On Sycamore Creek, three miles southeast of Fort Worth the Pawpaw has an average
thickness from several measurements of 7.5 meters (24.6 feet).
At the southern border of Tarrant County the Pawpaw 'is 12 feet thick
and is transitional to the marl facies. In northern Johnson County the
transitional zone continues and the section consists of clay mixed with
marl. Passing from the upper Noland's River southeast to Riovista the
section changes considerably, for from Riovista southward the marl facies
is found, with little clay and no ironstone; there is also a corresponding
change in the Pawpaw fauna.
SECTION OF BRANCH OF NOLAND'S RIVER NEAR CLEBURNE-WEATHER-
FORD ROAD, 10 MILES WEST OF CLEBURNE, TEXAS
Section furnished by W. M. Winton
MAINSTREET: Feet
Massive limestone containing Pachymya sp., Turrilites brazoensis, Holectypus
limitis, Pecten sp 32 . 4
PAWPAW:
Reddish clay containing fragments of Turrilites sp., Area sp., etc.. pyritized 10.8
WENO:
Limy marl capped by a hard lime ledge one foot thick, containing Pecten
georgetownensis, Nautilus texanus, Pinna sp., Kingena sp 7.8
34 University of Texas Bulletin
Marl, containing Nodosaria texana 1.0
Massive limestone containing Schloenbachia sp. M. (notched tubercles),
Nautilus texanus, Epiaster sp., Protocardia sp., Gervilliopsis invaginata
(one) * 7-4
CONCEALED BY BED OF STREAM, ESTIMATED 10.0
Soft whitish marl, no fossils seen 10.0
Marl Facies
The transition from clay facies to the marl facies of this formation takes
place rather abruptly, within a distance of 2 miles along the outcrop and
terminates in central Johnson County, south of which the formation is al-
most entirely marly. One mile southeast of Riovista, the Pawpaw is a dis-
tinctly marly uniform light yellow, fossiliferous deposit lying between the
conspicuous Weno and Mainstreet limestones. It is about 5 feet thick. In
the territory covered by this depositional phase the conspicuous pyrite fauna
of the Fort Worth region is rare, except a few Turrilites, Area and small
gastropods, and other fossils, echinoids and ammonites are abundant.
SECTION ON WACO-RIOVISTA ROAD, ONE MILE SOUTH OP RIOVISTA, TEXAS
MAINSTREET: Feet
Massive white limestone with characteristic Mainstreet fossils: Turrilites
brazoensis, Kingena, Exogyra, arietina. Exposed 5
PAWPAW:
Homogeneous calcareous, straw-yellow marl with a few ironstone and calca-
reous fragments, containing Enallaster bravoensis, E. wenoensis, E.
riovistae, Holaster sp., Epiaster wenoensis, Plicatula sp., *Flickia boesei,
'Schloenbachia, sp., *Turrilites sp., *Arca washitaensis 5.5
WENO:
Limestone escarpment in two terraces, poorly exposed at the base, consisting
of massive soft limestone with marl interbedding. Contains Enallaster,
Epiaster, Holaster, Hemiaster calvini, Pecten subalpinus, Plicatula and
many other fossils, Trigonia clavigera. About 40
DENTON:
Soft light straw-colored marl containing Gryphea washitaensis, Ostrea cari-
nata, Pecten subalpinus, Plicatula sp., and Kingena sp. (large) 5
LIMESTONE FACIES : The equivalents if any of the Pawpaw forma-
tion in Central Texas are largely insignificant since they consist of only a
minute thickness of very calcareous marl and limestone imbedded in the top
of the Georgetown limestone, underneath the Turrilites brazoensis zone
which represents the basal Mainstreet formation of North Texas. This sit-
uation presumably exists westward to the Trans -Pecos region wherever the
Weno and Pawpaw Formations 35
more southward section is found. However, in, West Texas, on passing
northward into the near-shore facies (as at Kent and Cerro de Muleros)
the Weno and Pawpaw formations again thicken, as in passing from Austin
to Fort Worth, and show characteristic and so far as can be judged from
published accounts .similar fossils. This level at Muleros has echinoids and
ammonites and other distinctive fossils (see page 41), but so far the large
pyrite fauna of the North Texas Pawpaw has not been reported from West
Texas.
WENO FORMATION
A summary of the marine facies of the Weno formation and several ge-
ological sections have already been given. The Weno formation is compos-
ite, and represents different phases of marine deposition both at different
places and in its different levels at the same place. In the Red River region
the formation is mostly a series of blue shales with clay-ironstone, lime-
tone and irregular consolidated sand seams. The ironstone and shale lay-
ers are rich in nacreous fossils. The shale is here capped by the Quarry
limestone group, which loses its massive character south of Denton County,
Passing southward from the Red River, the basal Weno transforms from a
clay into a calcareous marl with shelly, often slabby, limestone seams and
the upper part after passing rapidly through a marl stage becomes pre-
vailingly a soft chalky fossiliferous limestone. This is the situation in Den-
ton and Tarrant Counties. The basal division is also capped by a thin
chalky limestone which forms a bench, and the Weno thus consists of two
terraces, a persistent topographic feature which passes southwards across
Denton, Tarrant, Johnson and Hill Counties and disappears only in north-
western McLennan County where the Weno limestone consolidates with
the Mainstreet and Fort Worth limestones (by the virtual disappearance of
the intervening softer formations) to form the middle Georgetown lime-
stone.
In the Red River region the shale (clay) facies predominates from south-
ern Cooke County to east of Bennington, Oklahoma. It is conspicuous in the
first deep cut of the St. Louis and San Francisco Railway track north of
Denison, of which a photograph is given by Stephenson,1 and in the pit of
the brickyard 1% miles southeast of Gainesville ,of which a section is here
given.
'Stephenson, U. S. G. S., Prof. Paper 120-H, pi. XXII B.
36 University of Texas Bulletin
SECTION OF THE WENO FORMATION AT LOCALITY 601, PIT OF GAINES-
VILLE BKICK COMPANY, ONE AND THREE-FOURTHS MILES SOUTH-
EAST OF GAINESVILLE, TEXAS
PAWPAW: Feet
Shell limestone, consisting almost entirely of masses of comminuted shells. . . 0.2
Shelly calcareous marl, with ironstained arenaceous cement and masses of
shells. O. QUADRIPLICATA LAYER 8
This stratum contains: O. quadriplicata, Pecten subalpinus, Plicatula
sp., Leiocidaris sp. spines.
Hard reddish limestone composed almost entirely of- comminuted shells iron-
stained 3
Shell conglomerate of small packed shells, laminated .5
QUARRY:
Compact shelly blue to yellow limestone containing many comminuted shell
fragments. QUARRY LIMESTONE 9
This stratum contains: Gryphea sp., Pecten subalpinus, cidarid spines
(rare), Plicatula sp.
Shell conglomerate of Gryphea washitaensis chiefly, with considerable cal-
careous cement. GRYPHEA CONGLOMERATE 7
This stratum, which is conspicuous as just underlying the cap rock
of the rim of the pit, contains: Ostrea carinata, cidarid spines, Ostrea
marcoui, Plicatula sp.
WENO:
Packed bluish to yellow clay, with two thin seams of Gryphea shell conglom-
erate, each one inch thick 1.0
Sand layer containing no fossils, irregular thickness, about .2
Blue to yellow shale, with a considerable amount of sand in the form of
irregular anastomosing sand lenses and streaks. Fossils in the shale . . 4.7
Ironstone band .1
Blue to yellowish iron stained shale, with irregular calcareous concretions,
locally called "ginger shale" 2.5
The ginger concretions also occur in the sandy layer just above the
ironstone seam.
Fossiliferous Ironstone stratum .5
The clay-ironstone of this and the overlying ironstone layers has been
excavated and dumped in a large heap on the east rim of the pit.
Material in situ in the pit and that in this heap bears the following
nacreous fossils: %Protocardia sp. aff. multistriata (Shumard), very
abundant as casts and molds, with the original shell; $Barbatia sp.,
JCorftwto basiniformis Adkins, $Nucula nokonis Adkins, %-Nucula weno-
ensis Adkins, $Globiconcha sp., ^.Natica sp., \Cinulia washitaensis
Adkins, Cambarus (?) sp., %Schloenbachia wintoni Adkins, %Gervilliopsis
invaginata (White), %Pecten inconspicuus Cragin, $An,chura mudgeana
(White), and many other fossils.
Blue fossiliferous shale and calcareous bands 4.0
This material is an alternation of thin bands of yellow sandy lime-
Weno and Pawpaw Formations 37
stone with packed laminated blue-gray shale, slate color when fresh,
but weathering to blackish-blue.
Fossiliferous ironstone band .2
Blue shale, laminated, jointed on weathering, very fossiliferous 19.8
This layer contains an abundant nacreous shell fauna, including:
Gervilliopsis invaginata (White), Gryphea washitaensis Hill (juvenile
stages), Enallaster sp., Tellina sp., Corbula basiniformis Adkins, Nucula
wenoensis Adkins, Pecten inconspicuus Cragin, Anchura mudgeana
White, Natica sp., Turritella sp., Cerithium sp., etc.
Gray-blue arenaceous laminated shale, calcareous in part, forming a terrace
in the pit. G. washitaensis, Gervilliopsis invaginata, Pecten, Plicatula .3
Laminated blue shale '. .2
Ironstone seam .1
Laminated gray-blue shale 1.9
This works down into kidney-shaped lumps, and is locally called
"kidney shale."
Arenaceous laminated marl. Gryphea washitaensis abundant at top and
bottom. Main zone of Gervilliopsis invaginata (White), Trigonia clav-
igera Cragin, Pecten subalpinus Bose, Leiocidaris spines. This layer
forms a secondary terrace .8
Blue fossiliferous marl. Locally called "buff marl," a desirable brick ma-
terial, free from impurities, burns to buff color 11.2
51. C
This material has been thrown in heaps onto the terrace above and is rich in small
calcitic fossils, including: Venericardia wenoensis Adkins, Trochus laticonicus Adkins,
Trigonia clavigera Cragin, Neritina, Nerita, Pecten sp., worm tubes, minute corals
In the bottom of the pit covered by water is about 30 feet more of Weno shale.
It is stated that the pit has at one point been dug 70 feet deep. A water well
nearby passed through the Denton marl into the Fort Worth limestone. The Dentor,
marl is poorly exposed one-fourth mile west of the pit, and the Fort Worth limestone
is finely exposed with its typical sequence of fossil zones, in the creeks between th(
brickyard and Gainesville.
The Quarry limestone is variable in thickness. Blocks two to three feet
thick have been excavated from the pit and thrown in a heap above its
south rim. An extensive outcrop, with quarried indurated blocks, three
feet thick, occurs three miles east of Gainesville just north of the track.
The quarry group forms a persistent outcrop eastward to the river near the
the northeast corner of Graysoh County, in which county its relations
have been described by Stephenson. In Denton County on the Denton-
Krum road, it outcrops as a bench, and is 15 inches thick. Here it is
abundantly fossiliferous, and contains Pecten subalpinus, cidarid spines,
Ostrea marcoui, Gryphea washitaensis and Ostrea carinata. Beneath it
is a ferruginous and calcareous shell conglomerate layer 1 to 2 inches
thick consisting almost entirely of the last two species named. In Tarrant
38 University of Texas Bulletin
County it is consolidated with the top of the Weno formation, which is a
chalky limestone.
SECTION OF PAWPAW AND WENO FORMATIONS AT LOCALITY 602 ON
SYCAMORE CREEK, FOUR MILES SOUTHEAST OF FORT WORTH, TEXAS
MAINSTREET: Feet
White massive limestone, with Kingena wacoensis (?) (Roemer), Turrilites
brazoensis Roemer, Exogyra arietina Roemer, Pecten subalpinus (Bose),
Homomya, Pachymya, Ostrea carinata (?) Lamarck. Exposed 15.0
PAWPAW:
Marl and clay, with thin ironstone seams. The top marly portion contains
Enallaster sp., Hemiaster sp., Holaster sp., Epiaster sp., Pecten sub-
alpinus (Bose) and many other calcite fossils 18.0
Sandstone flag layer. STARFISH ZONE 3
Ironstained reddish impure clay with many pyrite fossils, including : Engon-
oceras sp., Turrilites sp., Hamites tenawa Adkins and Winton, Holaster
sp., Enallaster sp., Hemiaster sp. aff. bexari Clark, Acanthoceras
worthense Adkins, Area, sp., Nucula sp., Mortoniceras worthense Adkins,
Schloenbachia sp 4.0
WENO:
Impure limestone, forms top of first terrace. Marlier beneath, Nodosaria
texana Conrad, zone at the base 19.7
Limestone at top, forming second terrace, marl beneath. Contains a large
fauna, rich in echinoids and pelecypods. . . .• 31 . 0
Limestone ledge, indurated, fucoidal, Gervilliopsis invaginata (White) zone,
Gryphea washitaensis Hill, Pecten subalpinus (Bose), Pinna guada-
I it par Bose 1.3
There is about 13 feet of fossiliferous Weno marl beneath the creek bed. This is
well exposed at the locality 618 (q. v.).
SECTION OF THE WENO AND PAWPAW FORMATIONS FOUR AND ONE-HALF
MILES SOUTHEAST OF FORT WORTH, TEXAS, AND JUST NORTH OF
THE INTERNATIONAL AND GREAT NORTHERN RAILWAY BRIDGE
ACROSS SYCAMORE CREEK
MAINSTREET: Feet
White massive, in part marly, limestone, with Kingena (?) wacoensis
(Roemer), Exogyra arietina Roemer, Turrilites brazoensis Roemer,
Ostrea carinata Lamarck (?) 6.0
PAWPAW:
Brown clay, marlier ot the top, with an abundant pyrite fauna at the base,
including: Area sp., Mortoniceras worthense Adkins, Acanthoceras
worthense Adkins, Engonoceras sp., Schloenbachia sp., Hamites sp.,
Turrilites sp., Plicatula sp., Pecten subalpinus (Bose), Enallaster bravo-
ensis Bose, E. wenoensis Adkins, Epiaster wenoensis Adkins, and other
species 20.7
Weno and Pawpaw Formations 39
WENO:
Chalky limestone; contains: Ostrea sp. aff. diluviana, Ostrea curinata (?)
Lamarck, Pachymya austinensis Shumard, Homomya sp., Schloenbachia
sp. (M.), Pecten subalpinus (Bose), Pecten texanus Roemer, Plicatula
sp., Nodosaria texana Conrad, and many other species 13.5
Yellow marl with many limestone bands, poorly exposed 36.2
Hard white limestone, fucoid, with Gervilliopsis invaginata .5
Brownish yellow marl, about ' 15.0
SECTION OF PAWPAW AND WENO FORMATIONS EAST OF KATY LAKE
AND EAST OF SYCAMORE CREEK, ABOUT THREE AND ONE-HALF
MILES SOUTHEAST OF FORT WORTH, TEXAS
Section furnished by Gayle Scott
Section is from creek bed to upland; direction of section, 92 degrees from magnetic
north.
MAINSTREET: Feet
Weathered limestone : 15.6
Limestone ledge, with slight terrace above 2.7
PAWPAW:
Terrace, covered with soil and water-soaked, marl base; contains a sandstone
ledge two feet below top - 10.4
Red, ironstained, slightly sandy marl, with numerous small pyrite fossils;
characteristic weathering of receding Pawpaw hillsides 12.0
Yellow marl, in part soil-covered overlying the flat narrow terrace formed
by top member of Weno limestone L : 3.0
WENO:
Hard limestone ledge, partly concealed, about 3.2
Disintegrated thin limestone ledges alternating with marl layers of varying
thickness, partly concealed by limestone debris and soil 10.5
Limestone ledge, impure, yellow, heavily ironstained, indurated ledge, con-
taining Pentagonaster texensis Adkins and Winton (rare), and small
starfish, indet. (fairly numerous). This ledge forms the base of the
abrupt upper Weno terrace, and is easily recognizable in the Fort Worth
region. PENTAGONASTER ZONE 1.0
Yellow marl, heavily ironstained, containing thin limestone ledges. NODO-
SARIA TEXANA HORIZON 6.0
Disintegrated limestone, capped by a thin limestone ledge 3.2
CONCEALED. Interval contains Gervilliopsis Zone 28 . 5
Heavy limestone ledge, impure, fucoidal, yellow, and slightly less resistant
than the one mentioned below .9
Blue marl (pipe clay), weathering to gray, fractures on drying into small
blocks 3.5
Heavy limestone ledge, fairly pure, very resistant, containing Pecten texanus,
Pecten georgetownensis. In many places forms the bed of Sycamore
Creek 1.5
Blue marl (pipe clay), gray on weathering, and having a very fine texture 5.2
40 University of Texas Bulletin
DENTON:
Top of Gryphea washitaensis conglomerate, in bed of creek 2.0
Further sections of the Weno formation in Denton, Johnson, and other counties have
just been given in the discussion of the Pawpaw formation (q. v.).
STRATIGRAPHIC CORRELATION
NORTH CENTRAL TEXAS AND SOUTHERN OKLAHOMA
The Weno and Pawpaw formations can be traced continuously through
these two regions and their correlation is obvious. As has been already
noted, the sandstone facies of the Pawpaw formation has been included by
Taff in his Bokchito formation. This facies is similar at Gainesville, Den-
ison and Bokchito, and in itself affords insufficient differences to be con-
sidered as a different formation on the two sides of the Red River. The
whole Weno formation is also included in the Bokchito formation of Taff.
Taff's tabulation of equivalencies1 makes clear that the Bokchito forma-
tion is to be considered equivalent to the undefined upper part of the
Georgetown limestone in the Austin quadrangle, but to what formations
in North Texas is not clear. However, his Caddo formation is described
as having at its top a bed of oyster shells "similar to those occurring below
and at the top of the Kiamichi formation" (ibid, p. 6). This is the Den-
ton marl and has characteristic Denton fossils, and therefore the base of
the Bokchito formation is to be considered as the base of the Weno.2
SOUTH CENTRAL TEXAS
The Weno and Pawpaw formations have been traced with certainty to
the Brazos River south of Blum. The regional and facies differences in
Central Texas make correlation difficult on account of the smallness of the
known Del Rio fauna. It is presumed that the Exogyra arietina zone of
the basal Del Rio clay is continuous with that of the Mainstreet limestone
north of the Brazos near Blum, and that the Nodosaria texana zone present
in West Texas at the top of the Del Rio just beneath the Buda limestone1
but reduced or absent in Central Texas does not correspond to the promi-
nent Nodosaria zone found at the top of the Weno and the base of the Paw-
!Taff : Atoka Folio, p. 6.
2Stephenson (U. S. G. S., Prof. Paper 120-H, pi. XVIII) places the Denton clay
member and the Ostrea carinata bed capping it at the base of Taff's Bokchito forma-
tion; and also, very curiously, puts the "Gervilliopsis bed" near the base of the
Denton clay.
3B6se: Univ. Texas Bull. 1902, p. 19.
Weno and Pawpaw Formations 41
paw formations in North Texas. Turrilites brazoensis, also a fossil of very
limited vertical range, marks the top of the Georgetown limestone and
the base of the Del Rio clay in Central Texas from the Brazos southwards.
The basal Mainstreet then is represented by the uppermost Georgetown in
Central Texas, and the Pawpaw if present by strata lying high in the
Georgetown, while the bulk of the lower Del Rio (Exogyra arietina zone)
is Mainstreet and the upper Del Rio is Grayson.
WEST TEXAS AND MEXICO
West of the southern turning point of the Comanchean outcrops in Bexar
County, the Georgetown limestone and the Del Rio clay preserve their in-
dividuality into the Trans-Pecos region. At the type locality of the Del
Rio clay, it is typically developed as a laminated, greenish-blue clay with
thin instratified arenaceous clay seams, calcareous flags and shell breccia
(Exogyra arietina and Noslosaria texana) . In lithology this formation
"varies from a clay to an arenaceous thin bedded limestone."1 Here the
limestone facies is beginning to appear. It increases in amount south-
wards and in the Mariscal Mountains the bulk of the formation is lime-
stone. On the other hand, at Cerro de Muleros, Bose's subdivision 6, rep-
resenting Weno and Pawpaw, is a marl with sand and lime, and his sub-
division 7, representing the Mainstreet is sandstone. The lithological va-
riations of the Weno and Pawpaw are summarized on page 27. The
Georgetown, like the Buda, is over much of West Texas a fine grained
crystalline semi-lithographic limestone, grading northwards into a marlier
and sandier near shore phase. The same correlation as in Central Texas
(page 40) holds for these strata.
The age of subdivision 6 of Cerro de Muleros is delimited by several of
its fossils. The following fossils have not been found below this subdi-
vision, nor below the Denton formation in North Texas : Ostrea quadri-
plicata Shumard, Ostrea marcoui Bose. Pinna guadalupae Bose is un-
known below subdivision 6 and below the Weno of North Texas. Enallas-
ter bravoensis Bose, known from subdivisions 5-6, is not known to occur
lower than the Denton formation* elsewhere. Helicoctyptus mexicanus
Bose of subdivision 6 is as yet known only from the Pawpaw of North
Texas, and the same is true of Placosmilia spp., which are probably iden-
tical with P. bravoensis and P. mexicana. The zone of extreme abundance
of Gryphea washitaensis Hill so conspicuous in this subdivision is paral-
leled in North Texas only by that at the top. of the Denton formation.
'Roberts and Nash: Univ. Texas Bull. 1803, pp. 14-15.
42 University of Texas Bulletin
These facts indicate that subdivision 6 is equivalent to the Weno and
Pawpaw and to part of the Denton formation. The overlying sand, lack-
ing Exogyra arietina, contains near its top Hemiaster calvini Clark and
Exogyra whitneyi Bose. The former fossil is upper Washita, Weno to
Buda, and the latter is known from the Buda, although from the present
record it is evident that it ranges as low as the Mainstreet formation.
It may be of interest to add a list of species described from Cerro de Muleros, which
have been found in North Texas. The number cited is that of the corresponding divi-
sion at Cerro de Muleros, and the following formation names refer to the location
of the fossil in North Texas.
Epiaster aguilerae Bose, 5; basal Fort Worth.
Enallaster bravoensis 5, 6, 8; Weno to Grayson.
Holectypus limitis 5; Weno to Grayson.
Ostrea marcoui 4, 5, 6; Weno to Grayson.
Pinna guadalupae 2, 6; basal Weno.
Pecten subalpinus 2, 3, 5, 6, 8, 9; Goodland to Grayson.
Pecten irregularis 1, 2; Walnut to Kiamitia.
Plicatula subgurgitis 2, 5, 6 ; Duck Creek to Pawpaw.
Helicocryptus mexicanus 6; Pawpaw.
Turbo chihuahuensis, 'Lei Encantada; Weno.
Tylostoma chihuahuense 1, 2; Glenrose to Goodland.
Schloenbachia trinodosa 5, 6; Duck Creek.
EUROPE AND NORTHERN AFRICA
It is unquestionable that the aggregation of Pawpaw pyrite ammonites
here described parallels Pervinquiere's Vraconian fauna more closely than
it does his Cenomanian fauna. This might mean that the Pawpaw fauna
is Vraconian, or that some later (Cenomanian) species are included in his
Vraconian fauna; or the Pawpaw fauna may be one which has persisted
with little change from its Vraconian ancestors. Scaphites aequalis-like
species in Texas are known to range from the Duck Creek marl to at least
the Pawpaw clay; in Europe they are of Upper and Lower Cenomanian,
Vraconian, or even Albian age, so that this species decides little ; the Paw-
paw or the Duck Creek aequalis may be contemporaneous with the Vra-
conian examples. Flickia decides nothing, since the range of the genus is
unknown and is extended with each new species discovered. Hamites sim-
plex ranges from Aptien to Mid-Cenomanian. Attempts have been made
to correlate the Texas Washita division on the basis of Schloenbachia in-
flata. This brings us face to face with the question, What is inflata? Is it,
as sometimes claimed, a Schloenbachia with low, sigmoidal ribs and two
tubercles, one umbilical and one marginal; or is it a Mortoniceras, with
square volutions and coarse short ribs having three tubercles, an umbilical
Weno and Pawpaw Formations 43
and a pair of twinned ventro-marginal ones, as indicated by Pervinquiere?
If the latter, there is no Duck Creek species known to me that approaches
it as closely as do several Upper Washita species. For only above the base
of the Weno do we begin to find fairly large (6-12 inches) coarse straight
ribbed square coiled ammonites with an umbilical and a twinned marginal
tubercle ; this is the commonest and most characteristic Weno calcite spe-
cies, and it abounds in slightly smaller size in the nacreous ironstone Weno
fauna (Plate 3, figure 11). In the Pawpaw clay the same type is abun-
dant as small pyritic casts (M. worthense, Plate 1, figures 6-10, 18-19, 26),
having extremely short coarse ribs with very prominent twinned marginal
tubercles and a narrow square volution. Again in the Mainstreet lime
stone the common calcite species has lower, somewhat sigmoid ribs with
twinned marginal tubercles and a rectangular section. Are any of these
inflata? If the Vraconian is to be placed in the Weno, which seems pos-
sible, the whole Cenomanian will have to lie between the Pawpaw and the
base of the Eagleford shales, which is generally claimed to be the base of
the Turonian. Again a Duck Creek species similar to Schloenbachia elob-
iensis has been noted ; but a comparison of Szajnocha's figures and descrip-
tion indicate that this species is different from his ; its section is much lower,
and the shell bears spiral circlets which form regular radial rows contain-
ing numerous imbricated lips, while in the Texas species (known only as
internal casts) there are radial rows of only a few rounded tubercles; in
addition, the stratigraphic data given by Szajnocha are inadequate for cor-
relation with the Texas strata.
A comparison of the Duck Creek limonite fauna with the African Vra-
conian yields only slight results. On the theory that the Pawpaw is Vra-
conian, the Duck Creek could scarcely be placed earlier than the Albian,
since the Glenrose is with some certainty assigned to the Aptian. But Al-
bian species' are not apparent in the Duck Creek limonite fauna, whose am-
monites are preponderantly small species of Schloenbachia and Hamites,
with scattering Scaphites sp. aff. aequalis. Desmoceras, etc. Hoplites and
other abundant Albian genera are so far unknown. The fauna on the other
hand is predominantly Vraconian. This Vraconian aspect appears to end
with the Duck Creek limestone oj marl, since with the next limonite fauna,
that of the Denton marl, there seem to be some species with Cenomanian
affinities. Comparison of the Texas Washita faunae with those of Western
Europe, examples of which are before me, shows much less resemblance
than with the Northern African fauna. Common European species, as
Douvilleiceras mammilare, Schloenbachia varians, S. mantelli, and Holas-
ter subglobosus have no representatives in the Texas material so far
known. On the other hand, the Mainstreet, Grayson and Buda faunae are
listed among other places in: Tomitch: Contributions a la Connaissance de 1'etage
Albien dans le Sud-Est de la France. Le Mans, 1918.
44 University of Texas Bulletin
of a higher Cenomanian type, containing for example Codiopsis sp. aff.
doma, Tissotia spp., and Acanthoceras spp. ; and Berry states1 that the Da-
kota (Woodbine?) flora is of Turonian age.
On the whole then the Pawpaw fauna is placed provisionally as Ceno-
manian with much uncertainty as to its exact position. This question will
be settled when the rich ammonite faunae of the Lower Washita are crit-
ically studied. The Texas Comanchean sea was transgressive or at least
not regressive for a long period so that the relatively stationary shallow-
water conditions may not have encouraged a rapid evolution of these am-
monites; whatever the cause, they present notable similarities from the
earliest to the latest pyrite faunae known in the Texas Comanchean. On
the theory of persistent and nearly stationary species from Vraconian to
Cenomanian time some nearly similar species should be much extended ver-
tically in the Lower Washita sediments; further study of the proper ma-
rine facies of each stratigraphical level should reveal these and by filling in
the great gaps in our paleontological knowledge give a fairly complete
faunal succession. It is hoped that information on the extent of the various
marine facies in the Texas Comanchean formations will contribute to this
result.
•
PALEONTOLOGY
The rich Weno and Pawpaw faunae initiate a new group of species after
the considerable paleontological break which occurs at the top of the Den-
ton marl. The Werio formation, besides containing characteristic ammon-
ites, is notable in its marl facies for an exuberant echinoid fauna, and in
its shale facies for a great abundance and variety of distinctive cephalo-
pods, pelecypods and gastropods preserved with the original nacreous shell.
Certain elements of this nacreous fauna forcibly remind one of the Eocene
faunae, with which they have many genera in common. The fossils are
perfectly preserved, often with iridescent luster, and the original shell
shows the minutest details : in pelecypods, prodissoconch and other embry-
onic stages, ligament, and usually the finest features of dentition and ex-
ternal ornamentation ; in the cephalopods, the original pearly or iridescent
shell, and beneath this, finely preserved sutures etched into the ironstone
interior.
The Pawpaw formation on the other hand contains a diverse and char-
acteristic assemblage of small pyritic ammonites, echinoids, pelecypods,
iBerry: U. S. G. S., Prof. Paper 84, pp. 71, 128.
Weno and Pawpaw Formations
45
gastropods, corals and other fossils.1 This fauna has close resemblances to
that described by Pervinquiere- from the Vraconian of Tunis and Algeria,
a subject that will be considered later.
The later Washita seas were transgressing over extensive land areas
and a large numerical expansion in the marine fauna occurred, probably
in part in the invaded trough already described. In addition, the portion
of the ocean bottom which received the mixed clay and sand deposits was
probably at a moderate depth and not far offshore, and permitted a wealth
and variety of fauna. Note the complexion of life in the Pawpaw seas:
swarms of sharks and dogfish; a multitude of bottom-loving Crustacea,
small crabs and lobsters, echinoids, oysters and scallops ; sessile corals and
worms; pelagic protozoa; a few large, free-swimming nautili and irides-
cent-shelled ammonites, and a great diversity of small ammonites.
'THE WENO FAUNA
Of the large and well preserved Weno fauna only a few species have
been mentioned in the literature, as follows :
Hill3 listed the following fauna from the North Denison sands (=Weno) :
Axinea sp. Tapes sp.
Nuculaea sp. Turritella sp.
Corbula sp.
And the following from the Pawpaw shales and the North Denison
sands (not separated) :
Turritella sp. (predominant)
Corbula sp.
Axinea sp.
Volsella sp.
Tapes sp.
Cytherea sp.
Tellina sp.
Aricula sp.
Gervilliopsis or Gervillea
Area sp.
Nucula sp.
Ammonites emarginatus Cragin
Spherwdiscus belviderensis var.
eerpentinum Cragin
Trigonia emoryi Conrad
Pholadomya postextensa Cragin
Cyprimeria (large sp.)
Anchura mudgea.no, White
Lcda 2 spp.
Mactra sp.
Dentalium sp.
Scularia sp.
Ostrea quadriplicata Shumard
Pecten inconspicuus Cragin
Yoldia microdonta Cragin
Turritella seriatim-granulosa Roemer
Astarte sp.
throughout this paper an asterisk (*) preceding the name of a fossil indicates that
the fossil has pyrite, limonite or hematite preservation; a double dagger (J) indicates
nacreous preservation.
2Pervinquiei-e: fitudes de Paleontologie Tunisienne. Paris, 1907.
••'Hill: Bull. Geol. Soc. Amer., 5, 1894., and 21st Ann. Kept., U. S. G. S. pt. 7, p. 277,
1901.
46 University of Texas Bulletin
The following species of the fauna have been described by Cragin:1
Pecten inconspicuus Tellina subaequalis
Pholadomya postextensa Sphenodiscus emarg'.natits
Corbula crassicistata Engonoceras belviderensis var. serpen-
Tapes denisonensis tinum
The following species were listed by Stephenson:2
Nucula sp. Cymbophora sp.
Ostrea quadriplicata Shumard Turritella sp.
Protocardia texana (Conrad) Anchura mudgeana White
Cyprlmeria sp. Engonoceras serpentinum Cragin
Corbula 3 spp. Crustacea
An incomplete list of the Weno fossils on hand is given in the accompany-
ing table (Table 1) ; many species were omitted for further study.
RANGES OF WENO FOSSILS
The range as given in this table will demonstrate that one of the major
paleontological breaks in the Washita division lies at the base of the Weno
formation. The contact between the Denton and Weno formations is ap-
parently conformable, and many species cross it ; but a considerable num-
ber of others do not range higher than this contact while another consid-
erable group does not range lower. Without speculating as to the origins
of the latter group, it may be delimited more closely in view of a more
detailed study.
ABBREVIATIONS FOR TABLE OF WENO FOSSILS
* Pyrite, limonite or hematite preservation.
I Nacreous preservation.
A Abundant
0 Occasional
R Rare
S Sand phase
SH Shale phase
M Marl phase
L Limestone phase
u upper part of formation
m middle
1 lower
1 Cragin: Colo. Coll. Stud., 5, 1894, p. 49.
2Stephenson: U. S. G. S., Prof. Paper 120-H, 1918, p. 141.
Weno and Pawpaw Formations 47
601 Pit of Gainesville Brick Company, brickyards one and three-fourths miles south-
east of Gainesville, Texas, just east of Rock Creek (branch of Pecan Creek)
and just south of the Missouri, Kansas and Texas railway (Wichita Falls
branch). Includes the ironstone dump on east rim of pit. Shale faciee
basally; ironstone and sand facies above.
602 East bank of Sycamore Creek, two and one-half miles southeast of Fort Worth,
Texas. Marl facies basally; limestone facies above.
604 Cut of St. Louis and San Francisco railway, three-fourths mile north of Union
Station, Denisoh, Texas. Shale facies basally; ironstone and sand facies
above.
605 A branch of Duck Creek, three-fourths mile north of Union Station, Denison.
Texas, and just west of locality 604. Shale facies.
606 Exposure in valley just south of St. Louis and San Francisco track, two miles
north of Denison, Texas. Shale facies.
611 Waterfall 200 yards south of crossing of International and Great Northern rail-
way over Houston and Texas Central railway track near Sycamore Creek,
three miles southeast of Fort Worth, Texas. Marl facies.
612 Cliff on northeast bank of Sycamore Creek, 100 yards north of the Houston and
Texas Central railway bridge across Sycamore Creek, three miles southeast
of Fort Worth, Texas. Marl facies basally; limestone facies above.
618 Area in valley east of Armstrong Iron Works, South Hemphill street, Fort
Worth, Texas, and west of the International and Great Northern railway
track. Marl facies basally; limestone facies above.
THE PAWPAW FAUNA
As already stated, the bulk of this fauna is limonitic, pyritic or hema-
titic, but there are in addition some fossils with calcareous preservation.
The calcareous fossils are echinoids, pelecypods, a few cephalopods and
other miscellaneous fossils. The echinoids of the basal portion of the for-
mation are mainly limonitic, but those of the upper, marlier portion over
all of the Pawpaw outcrops except in the Red River region, are calcareous
mud-filled tests.
LIST OF PAWPAW LOCALITIES
714 One-fourth mile south of the International and Great Northern railway bridge
across Sycamore Creek, four and one-half miles southeast of Fort Worth,
Texas. Entire thickness of Pawpaw, somewhat overwashed at top; north-
eastward facing slope of hillside, and beneath the slope a considerable terrace
on the top of the Weno limestone. Clay facies basally; some marl at top.
716 Amphitheater one-half mile northeast of locality 714. Entire thickness of Paw-
paw formation exposed.
716 Pit of Cobb Brickyards, one-fourth mile east of Sycamore Creek and three miles
southeast of Fort Worth, Texas.
718 Cut of International and Great Northern railway track one-fourth mile south of
bridge across Sycamore Creek, four and one-half miles southeast of Fort
48
University of Texas Bulletin
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GASTROPODA :
' jCinulia washitaensis Adkins..
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PELECYPODA:
tGervilliopsis invaginate (Wh
Pecten subalpinus (Bose)
— texanus Roemer
— georgetownensis Kniker
Gryphea washitaensis Hill
Ostrea quadriplicata Shumard
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50
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Weno and Pawpaw Formations 51
Worth, Texas, and one-eighth mile east of locality 714. Upper part of Paw-
paw formation, partly marl, overlain by Mainstreet limestone.
719 Crowley Road, one mile south of the Baptist Seminary, and four! and one-half
miles south of Fort Worth, Texas. Westward facing cut in hillside, exposing
poorly most of the Pawpaw formation.
720 Rim of Weno escarpment one mile southeast of Riovista, Texas, and midway
between the Riovista- Waco pike and the Santa Fe track. The Pawpaw, simi-
larly exposed between the Mainstreet and Weno limestones, continues west-
ward to the next locality.
721 East-west escarpment just east of Riovista-Waco road, one mile south of Riovista,
Johnson County, Texas. The Pawpaw is much thinned, and is transitional
between clay and marl facies.
722 Cut of Missouri, Kansas and Texas railway (Wichita Falls branch) at north
end of pit of the Gainesville Brick Company, one and three-fourths mile?
southeast of Gainesville, Texas.
723 Westward facing hillside lying under Mainstreet upland on west side of Mans-
field Road, halfway between Glen Garden Country Club and Sycamore Creek,
three miles southeast of Fort Worth, Texas.
724 Hillside on north side of east-west road, three miles southeast of Haslet, Tarrant
County, Texas. Whole thickness of Pawpaw.
FAUNA OF THE PAWPAW FORMATION
S : Sand facies ; C : Clay facies : M : Marl facies : L : Limestone facies ; A : Abundant : O : Occasional :
R: Rare; 1: lower third of Pawpaw iteration ; m: middle portion of Pawpaw formation; u: upper portion
of Pawpaw formation ; * : Pyrlte or limonite preservation ; } : nacreous preservation.
SPECIES LOCALITY :
CEPHALOPODS:
716
C
R
714
C
R
716
C
R
718 719
M C
O
728
C
R
724 722
CS S
720 721
M M
R R
R
R
O
R
R
R
•FHckia boeaei Adkins ._
Rl
A
A
O
O
A
O
A
A
R
R
R
R
Ol
O
O
A
R
Ol
O
R
O
•Turrilites worthensis Adkins and Winton
•Turrilites sp. B. Adkins and Winton
A
O
A
A
A
A
A
O
A
O
A
A
A
A
R
O "
—
R
R
R
O
0
O
A
O
O
A
R
A
A
A
O
A
O
tEnponoceras serpentinum Craftin
R
R
R
R
--
R
R
R
ASTEROIDEA :
Rl
*M t t AHk* A W' t
Rl
R
•T P ^ ^ !_r "^AHk"
Rl
• d t
Rl
OPHIUROIDEA:
OnhioelFDha sn. -
R
52
University of Texas Bulletin
SPECIES LOCALITY :
ECHINOIDEA :
716
714
R
715
718
719
723
724
722
720
721
*P*»ltfl8t'*& 8P
R
O
O
O
O
o
o
O
o
o
O
o
o
o
O
A
A
O
o
O
o
O
o
O
O
o
o
o
o
O
o
o
o
o
O
o
o
o
o
o
R
o
o
o
O
o
o
O
O
R
A
o
R
CRUSTACEA :
R
R
R
R
CORALS :
R
R
R
R
R
PROTOZOA:
o
A
o
o
O
0
PELECYPODS :
A
A
A
A
A
R
o
O
O
O
O
o
0
0
O
O
0
R
R
R
R
p^m°n,la *
A
A
A
A
A
A
A
A
R
R
R
O
O
O
O
O
0
0
T d
O
O
O
R
T .
O
A
A
0
O
GASTROPODS :
R
O
R
O
O
R
o
O
R
R
R
R
R
O
R
O
R
VERTEBRATES :
ft
R
SP" '(OH t ' d' ul tus?)
A
A
A
o
0
A
O
A
A
A
A
O
A
0
an. indet. (vertebrae) _
A
A
A
A
_
A
—
0
—
PARALLELS BETWEEN UPPER WASHITA AND LOWER WASHITA
ECHINOIDS
LOWER WASHITA
(below Weno formation)
Holectypus planatus Roemer
Enallaster texanus Roemer
Hemiaster whitei Clark and E. elegans
Shumard
UPPER WASHITA
(Weno and higher formations)
H. limitis Bose
E. bravoensis Bose
E. riovistae Adkins
E. wenoensis Adkins
E. sp. aff. texanus Roemer
H. calvini Clark
'Weno and Pawpaw Formations 53
Epiaster aguilerae Bose E. wenoensis Adkins
Holaster simplex Shumard H. sp.
Cyphosoma texana Roemer C. volanum Cragin
Salenia mexicana Schlueter and S. texana
Credner S" V°lana Whlt"ey
Goniopygus sp. G. budaensis Whitney
Goniophorus sp. 1 G. sp. 2.
COMPARISON OF PYRITE FAUNA
TEXAS
It has been pointed out' that the North Texas Comanchean system con-
tains a series of alternate lime and marl (or clay) formations, some of
which contain conspicuous pyrite and limonite faunae ; these are
(1) The Kiamitia formation;
(2) The Duck Creek marl;
(3) The Denton marl;
(4) The Pawpaw clay;
(5) The Grayson formation;
(6) The Del Rio clay.
Many pyrite and limonite species are common to these six formations,
and still others have more restricted vertical ranges and are confined to
limited levels within a single formation. In general it may be said that
these fossils are of distinct species from those otherwise preserved in the
same formation ; that they are rare in the intervening formations, and that
the complexion of the limonite faunae is different from that of the other
faunal components of the formations in question. In addition there seem
to be certain limonite species in the various intervening limestone forma-
tions, especially in the Fort Worth and Weno limestones. To assist in de-
termining the age and correlation of these formations the following pro-
visional fossil lists are given. The list for the Pawpaw formation will
be found on page 51.
The rather regular alternation of marl (or clay) and lime formations
in the North Texas section suggests some form of cyclic deposition, in
which the same marine conditions were many times repeated, and this
inference is equally strong for the contained pyrite faunae, when it is
found that they occur prevailingly in the alternate, clay, formations. This
'Winton and Adkins: The Geology of Tarrant County, Univ. Texas Bull. 1931.
1920.
54 University of Texas Bulletin
does not imply that in certain formations no pyrite faunae will be found ;
they existed somewhere during the whole Washita at least, and likely will
be found in the clay facies of each formation, just as representatives of
the Mainstreet pyrite fauna have been found in the clay facies (Del Rio)
of Central Texas, though apparently absent in the limestone of North Texas.
It is certain that exuberant pyrite faunae are associated with clay facies ;
and accordingly the greatest abundance of pyrite fossils in the Kiamitia
is in southern Tarrant and Johnson counties ; Denton formation, Denison
to northern Tarrant County; Pawpaw formation, Tarrant County; Main-
street formation, McLennan County and southward ; middle Grayson form-
ation, Denton County. In each instance the lithology of the region men-
tioned is largely of the clay facies. These facts suggest recurrent similar
conditions which favored the spread of pyrite faunae. At a given locality
this recurrence might be many times repeated ; and such pyrite zones are
still being discovered at new stratigraphic levels. What these conditions
and their causes were will not be discussed here. They resulted in each
zone in a highly characteristic pyrite and limonite fossil association, which
is as follows: Area washitaensis, Engonoceras sp., Scaphites spp., Tur-
rilites spp., Hamites spp., Cinulia sp., Nerinea sp., Lunatia sp., Turritella
sp-, pyritic starfishes, and abundant small, non-pyritic Crustacea, especially
crabs.
KIAMITIA CLAY FAUNA
The marl facies of the Kiamitia formation extends from Primrose,
southwest of Fort Worth, to a point between Gainesville and Fink, on
the Red River. The clay facies extend from near Primrose to at least
the Brazos River ; it is found throughout Johnson County, and on Cedar
Creek near Blum is a reddish clay 19 feet thick. With the advent of
the clay facies the shell conglomerates of the northern section disappear
and a pyrite fauna similar to that of the Duck Creek marl appears. This
little investigated fauna contains Area sp., and other small pyritic and
limonitic pelecypods and gastropods.
DUCK CREEK MARL FAUNA
This fauna is notable for its large number 'of small pyritic and limo-
nitic gastropods and pelecypods. Such genera as Cerithium, Cinulia,
Turritella, Turbo, Lunatia, Area, Nucula and Corbula are highly char-
acteristic of the lower Washita pyrite zones. Equally characteristic if
*
Weno and Pawpaw Formations »{>
the exceptional variety of gerontic ammonites, especially Hamites; Scaph-
ites, Schloenbachia, Desmoceras and other genera are also prominent in
the fauna.
DUCK CREEK LIMONITE AND PYRITE FOSSILS
*Scaphites worthensis Adkins and Winton.
*Scaphites sp. aff. worthensis.
*Engonoceras sp.
Hamites tanima Adkins and Winton.
•Karaites spp.
*Crioceras (?) sp.
•Schloenbachia sp.
*Neolobites (?) sp.
*Arca sp.
*Nucula sp.
*Turbo sp.
*Lunatia sp.
*Cerithium sp.
*Nerinea sp. aff. pellucida Cragin
*Cinulia sp.
*Anchura sp.
*Turritella sp.
*Nerinea sp.
*Placosmilia sp.
DENTON CLAY FAUNA
The clay facies of the Denton formation extends from northern Tar-
rant County (Blue Mound, near Haslet) to beyond Denison. It is char-
acterized by a great diversity of small pyrite and limonite ammonites,
some of them nacreous, and by many small Crustacea, mainly small pyritic
crabs. The ammonites seem more abundant southwards than on the
Red River and the Crustacea the reverse.
FAUNA OF THE DENTON FORMATION
* Limonite or pyrite species.
U Upper.
L Lower.
*Acanthoceras sp. aff. aumalense Coquand
*Engonoceras sp.
*Mortoniceras sp.
56 University of Texas Bulletin
*Schloenbachia sp.
*Acanthoceras (?) sp.
"Turrilites sp. (?)
*Baculites (?) sp.
Ophioglypha texana Clark
*Starfish sp. (ray)
*Goniophorus (?) sp. 2 specimens, one with the shell.
Leiocidaris sp. (spine and plate).
Leiocidaris hemigranosus Shumard.
Hemiaster sp. (plate).
Hoploparia sp.
Cambarus (?) sp. (like sp. in Gainesville brickyards Weno).
Crabs 9 spp.
Ostrea quadriplicata Roemer.
Ostrea carinata Lamarck.
Gryphea washitaensis Hill.
Ostrea sp. (small zigzag).
Stearnsia robbinsi White (?).
Gervilliopsis invaginata White (?)
Trigonia emoryi Conrad.
Plicatula dentonensis (?) Cragin.
*Arca sp.
Anomia sp.
Plicatula spp.
*Nucula sp.
*Cardium sp.
*Leda sp.
*Corbula sp.
Pecten sp. aff. inconspicuus Cragin.
Crania sp.
Dentalium sp.
?Porocystis-like masses.
*Natica sp.
*Cinulia sp.
Fish teeth, vertebrae, skin, plates.
GRAYSON FAUNA
The pyrite and limonite fauna so far discovered in the Grayson forma-
tion is confined to the middle clay member of the formation in North
Texas, and includes diverse ammonites, gastropods and pelecypods, as
listed below. However, the pyrite fauna of the middle Del Rio clay
which occurs in McLennan County and southward is of Grayson age,
Weno and Pawpaw Formations 57
and contains some identical species. This latter fauna is well developed
on the South Bosque River, five miles west of Waco and includes Turrilites
bosquensis Adkins, Flickia ( ?) bosquensis Adkins, Acanthoceras worth-
ense Adkins, Schloenbachia spp. and other common Grayson and Pawpaw
pyrite species. It is notable that the preservation of this fauna is almost
exclusively pyritic.
FAUNA OF THE GRAYSON MARL
* Pyrite or limonite species.
(C) Cidarid zone.
(Co) Coral zone.
U Upper member.
M Middle member.
L Basal member.
CEPHALOPODS:
Turrilites sp. (medium size) (M).
"Turrilites sp. aff. worthensis A and W.
*Turrilites spp. (M).
*Turrilites sp. (whiplash) (M).
*ammonite aff. Flickia (small, keelless) (M).
*Hamites 3 spp. (M).
Acanthoceras ? sp. (Denison, WSA).
Acanthoceras spp.
Engonoceras spp. (L).
*Schloenbachia spp.
ECHINODERMS:
Hemiaster calvini Clark,
starfish sp.
Goniophorus (?) sp.
cidarid spines 3 spp. (C).
Cyphosoma volanum (?) Cragin.
Enallaster texanus (?) Roemer.
Enallaster sp. aff. traski (?) Whitney.
Enallaster sp. aff. bravoensis Bose (?).
CORALS:
•Placosmilia (?) sp. (Co).
GASTROPODS:
Cerithium sp.
Turritella marnochi (?) White.
Turritella sp.
Cinulia pelletti Whitney.
*Gyrodes (?).
"Turbo sp.
•Turritella sp. (sharp spired) M.
58 University of Texas Bulletin
PELECYPODS:
Gryphea mucronata Gabb.
Gryphea sp. aff. corrugata Say.
Exogyra sp. aff. columbae Sowerby (L).
Exogyra n. sp. (Denison, M).
Exogyra sp. aff. texana (U, under Buda limestone, Bosque River, W of Waco).
Pecten texanus Roemer.
Pecten subalpinus Bose.
*Arca sp.
Ostrea sp. aff. subovata Shumard.
Lima sp. (elongate).
Lima sp. (quadrate).
Lima sp. aff. wacoensis Roemer.
Ostrea sp. (saucer).
Anomia sp.
Plicatula spp.
Protocardia texana (?) Conrad.
Pholadomya shattucki Bose.
Tapes sp.
Inoceramus sp. M.
Corbula (?) sp.
Trigonia sp.
Cyprimeria sp. (small).
Cyprimeria sp. aff. crassa Meek.
*Nucula sp.
*Crassatella (?) sp. ("Remondia").
*Barbatia sp.
Trigonia sp. (large).
*Isocardia sp.
Shark teeth, vertebrae, bones.
DEL RIO CLAY FAUNA
The Del Rio limonite fauna is very widespread in Texas, having been
found at Waco, South Bosque, Austin, Quihi (Medina County), Del Rio,
Terlingua, and the Solitario.
In McLennan County at the base of the Del Rio clay, which corresponds
to the middle of the Mainstreet limestone, an extensive pyrite and limonite
fauna occurs, including the following:
*Exogyra arietina Roemer.
*Turritella sp.
*Cerithium sp.
*Turrilites spp.
*Schloenbachia sp.
Weno and Pawpaw Formations 59
*Nerinea sp.
Lunatia sp.
•Natica sp.
Goniophorus sp.
Pecten subalpinus Bose.
Turrilites brazoensis Roemer.
The Del Rio pyrite fauna corresponding to the base of the Grayson
formation of North Texas has already been noted; it includes:
* Turrilites bosquensis Adkins.
*Flickia (?) bosquensis Adkins.
•Acanthoceras worthense Adkins.
*Schloenbachia sp.
Exogyra arietina Roemer.
Gryphea mucronata Gabb.
Gryphea sp.
Pecten subalpinus (Bose).
The first named limonite fauna with an extensive calcite microfauna
immediately overlies the Georgetown limestone and is of middle Main-
street age. It is seen at South Bosque, and will probably be discovered
at many places in Central Texas.
Liddle states that the Del Rio clay throughout Medina County, contains
great amounts "of dark brown limonitic fragments and fossils.' Good
localities are a small Del Rio inlier four miles slightly west of north of
Quihi on the Bandera road, and the main area of exposure just north of
the inlier. These localities contain limonitic gastropods, *Turrihtes, *Sca-
phites, small ammonites, and loose *Nodosaria.
At Loma de la Cruz and other localities in the Del Rio clay lowland two
miles south and southeast of Del Rio, the basal clay contains limonitic
*Schloenbachia sp., *Hamites sp., *Scaphites sp., *Turrilites (two species),
*sp. aff. Flickia ( ?) bosquensis Adkins ; *Pyrina or Cassidulus sp., cidarid
sp., *Leda (two species) , *Nucvla sp., *Arca sp. *Plicatula sp. ; *Nerinea
sp. (abundant), *Cerithium spp. and other fossils.
Along the base of the Reed Plateau, Terlingua, the basal Del Rio clay
contains abundant brown limonite fossils, the great majority of which are
various species of Turrilites. The fauna includes : *Nodosaria texana
Conrad, *T:irrilites (three species), * Acanthoceras sp., *Schloenbachia sp. ;
*Nucida sp.
'Liddle, The Geology and Mineral Resources of Medina County, Univ. Texas Bull,
(in press).
60 University of Texas Bulletin
The Del Rio clay surrounding the Solitario Uplift contains a rich assort-
ment of brown limonitic fossils, including *Engonoceras sp., *Turrilites
(two species), *Turritella sp., gastropods, *Nucula sp., *Tapes sp., *Nodo-
saria texana Conrad, and other fossils.
It may be mentioned that these limonite faunae in Texas are not confined
to the Comanchean, since & rich fauna was found in the Terlingua beds
(Taylor marl equivalent) about five miles north of the crossing of the
Alpine-Terlingua road through Terlingua Creek, Brewster County, Texas.
This fauna includes: *Turrilites sp., *Baculites sp., *Ptychoceras sp.,
*Desmoceras sp., *Trochosmilia sp., *Lingula sp., *Lunatia sp., *Natica sp.,
*Nerinea sp., numerous other gastropods, and fish teeth and vertebrae.
Bose1 found a rich Vraconian fauna in limestone blocks covering small
hills just west of Camacho, Zacatecas, between this station and the Trin-
idad mine, and west of Opal, Zacatecas, iri the core of an anticlinal hill
consisting of thin-bedded limestone with lenses and concretions of chert.
These fossils are mainly silicified, but are! cited here on account of their
striking resemblances to the pyrite fossils described in this paper. The
fauna includes typical Vraconian genera, as Phylloceras, Lytoceras, Macro-
scaphites, Hamites, Hamulina, Ptychoceras, Diptychoceras, Anisoceras,
Turrilites, Baculites, Desmoceras, Acanthoceras, Ancycloceras, Toxoceras,
Crioceras, Scaphites, Schloenbachia, Brancoceras and Exogyra.
SUMMARY OF PYRITE FAUNAE .
The Washita marl and clay faunae contain distinctive assemblages of
ammonites, Crustacea, starfishes, echinoids, gastropods, pelecypods, corals,
and other fossils. The Crustacea are preserved partly with the original
integument and partly with limonite replacement. The other fossils are
in part calcitic, but mainly limonite and hematite pseudomorphs and casts
of the interior of the -original shell.
Ammonites: These are very distinctive for each fauna. Species of
Schloenbachia abound in each marl and clay formation. Acanthoceras is
found in the Denton, Pawpaw and Grayson faunae, but not in the Duck
Creek. Hamites are abundant in the Duck Creek marl and present in
the other formations. Turrilites abounds in the Pawpaw and is not
known with certainty below it. Flickia, Hamulina, Baculites and Puzosia
are known only from the Pawpaw clay.
ose, On some new Cretaceous Faunas from Mexico, Univ. Texas Bull, (in press).
Weno and Pawpaw Formations 61
TABULATION OF KNOWN AMMONITES OF THE WASHITA PYRITE AND
LIMONITE FAUNAE
Species
Hamites
Duck Creek
marl
10
Number i
Denton
marl
1
jf Known J
Pawpaw
clay
3
Ipecies in:
Grayson
marl
3
Del Rio
clay
Turrilites
1?
10
4
1
Acanthoceras
2
2
1
1
Scaphites
2
2
Flickia
1
1?
Baculites
1
Schloenbachia
3
1
2
2
1
Mortoniceras
1
2
Puzosia . .
1
Hamulina
1
Engonoceras
1
1
3
1
Crioceras (?)
1
Neolobites (?) .
1
ECHINODERMS:
TABULATION OF THE KNOWN ECHINODERMATA OF THE WASHITA
LIMONITE FAUNAE
Number of Known Species in:
Duck Creek
Denton Pawpaw
Grayson Del Rio
Species marl
marl clay
marl clay
ASTEROIDEA:
Metopaster
1
• • • •
Comptonia
1
• • • •
Pentaceros
1
. .
genus, indeterminate..
1 2
1
OPHIUROIDEA:
Ophioglypha
1
..
ECHINOIDEAi;
Holaster 1
2
1
Hemiaster 2
1? 2
2
Stenonia
* • • •
1
Epiaster
1
Enallaster 1
3
3
Goniophorus 1
1 1
1? 1
Goniopygus
1
..
Leiocidaris
1
. .
Salenia
1
. .
cidarid spines
2
3
'Most of these haVe calcitic preservation.
62 University of Texas Bulletin
Of these echinoderms the starfishes and brittle stars have so far been
found only in the upper formations, Denton and above. The echinoids
also seem more abundant and varied in the Upper Washita; Enallaster
particularly shows a development of several species in the Weno and
Pawpaw formations. Stenonia supernus (Cragin) is known only from
the Grayson marl. Among the small echinoids, Regularia, especially
Salenidae, predominate. The Salenidae have a wide distribution and
their various species seem reliable as horizon markers.
CRUSTACEA :
There is a great variety of crabs belonging to many different genera.
Of the lobsters a small species of Hoploparia is abundant in the Denton
marl. Segments of appendages abound in these four formations; claws
are found in the Duck Creek and Pawpaw and rarely in the intervening
formations. These Crustacea are for the most part calcareous and ex-
cellently preserved. In addition there are known in the Texas Coman-
chean, from the Goodland indeterminate limb segments; from the Duck
Creek limestone Callianassa sp. claws; from the Fort Worth limestone a
lobster related to Homarus (Dr. Shuler) ; and from the Weno, two lob-
sters and an indeterminate claw. A crab and a lobster claw have been
reported from the Buda.
TABULATION OF KNOWN CRUSTACEA OF THE WASHITA PYRITE AND
LIMONITE FAUNAE
Duck Creek Denton Pawpaw Grayson
Species marl marl clay marl
ASTACURA:
Cambarus ? . . . 1
Hoploparia 1 1
appendages, indet , . . . . . . . 3
species, indet . . . . 4
ANOMURA:
Callianassa . 1
BRACHYURA:
species indet.
PELECYPODA :
The Duck Creek limonite fauna is marked by the relative poverty of
pelecypods and the relative abundance of gastropods. A small species
of Area, abundant in the Pawpaw also occurs in the other formations.
Weno and Pawpaw Formations 63
The Pawpaw and Grayson each has a considerable assemblage of small
pyritic and limonitic pelecypod casts.
TABULATION OF KNOWN PYRITE OR LIMONITE PELECYPODS IN THE
WASHITA PYRITE FAUNAE
Duck Creek Denton Pawpaw Grayson
Species marl marl clay marl
•Area 1 1 1 1
•Nucula 1 1 1 1
*Leda . . 1 1
"Corbula .. 1 1
*Plicatula 1221
*Barbatia . . . . ". . 1
*Isocardia (?) .. .. .. 1
*Remondia (?) .. .. 1 1
•Lima 1 1 2 1
GASTROPODA :
As may be seen in the following table, a fauna of small gastropods is
a feature of the pyrite and limonite fossils in these four formations. In
the Duck Creek marl these small limonite gastropods are the most con-
spicuous element of the fauna.
TABULATION OF WASHITA LIMONITE AND PYRITE GASTROPODS
Duck Creek Denton Pawpaw Grayson
Species marl marl clay marl
•Natica 1 1 1 1
•Cinulia 1 1 1 1
*Cerithium 1 . . . . 1
•Turritolla 1 .. 1 2
*Gyrodes 1 .. .. 1
•Turbo 1 .. 1 1
•Lunatia 2 .. 1
*Nerinea 2 . . 1
*Anchnra . 1
OTHER COMPONENTS:
Small corals (Trochosmilia, Placosmilia) occur in the Duck Creek and
Pawpaw formations, and probably in the Denton and Grayson. There is
a notable abundance of small sharks (Lamna, Oxyrhina, Ptychodus) in
the Pawpaw, where teeth, vertebrae, plates, skin and bones are found ;
the same fossils are found less abundantly in the other formations in
64 University of Texas Bulletin
question. These sharks also occur in the intervening limestone forma-
tions but their abundance in the marls and clays testifies to the favorable
conditions for their existence.
In view of the importance which these pyrite faunae may have for
correlation purposes, it is considered useful to refer to certain pyrite
faunae of approximately the same age known from Europe and Africa.
Of these the Vraconian fauna investigated by Pervinquiere shows the
closest similarities to the Pawpaw fauna here described, notably in the
ammonites. The bearings of these fossils on the correlation of the Paw-
paw formation have been discussed elsewhere (page 42). It is evident
that unless conditions for the pyritization of fossils are worldwide at
a given time, it is useless to attempt to make exact correlations of Texas
pyrite zones with particular zones abroad. Instead, those pyrite fossils
which have limited vertical ranges may, like any other such fossil, be
used to mark within narrow limits the age of the zone in which the fossil
occurs. A list of similar Texas and foreign pyrite and limonite species
is added.
EUROPE AND AFRICA
European Limonite and Pyrite Faunae1
VALANGIAN
Sayn2 has described a series of pyritic ammonites from the Valangian of Provence
and Dauphine; this fauna consists prevailingly of species of Lytoceras, Phylloceras,
Garnieria, Neocomites, Thurmannia, Mortoniceras and Leopoldia.
ALBIAN
In the Haute-Marne, near Montierender are two gray sand layers with pyritic
ammonites, separated by one meter of clayey sand.
Upper Level:
Lower Level:
Hoplites deluci
denarius Desmoceras beudanti
splendens Hoplites deluci
auritus denarius
Turrilites catenatus quercifolius
Hamites rotundus Douvilleiceras mamillatum
lyelli
Inoceramus concentricus Hamites alternotuberculatw
Nucula pectinata Belemnopsis minimus
iHaug: Traite de Geologic, pp. 1232-1298.
2G. Sayn, Les ammonites pyriteuses du sud-est de France. Mem. Soc, Geol. France.
No. 23, 1901.
Weno and Pawpaw Formations 65
Inoceramus concentricus
salomonis
Plicatula radiola
Nucula pectinata
Area fibrosa
Trigonia fittoni
Dentalium decussatura
Solarium moniliferum
Cerithium trimonile
A.LBIAN
In the Rhone basin (les Baronnies and le Diois) the Albian is bathya] and contains
a level of small pyritic ammonites:
Phylloceras alpinum
Tetragonites timotheanus
Kossmatella chabaudi miihlenbecki
Desmoceras latidorsatum
VRACONIAN
In the Rhone basin, region of Dieulefit, the Vraconian is represented by black marls
with pyritic fossils:
Gaudryceras dozei
Turrilites bergeri
tuberculatus
Belemnopsis ultimus
Cerithium lallerianum1
Avellana muratelli
African Pyrite Faunae
ALBIAN
In the province of Constantine Blayac2 collected the following species, preserved as
ferruginous molds:
Upper Level: Lower Level:
Tetragonites timotheanus Phylloceras velledae
Kossmatella agassiziana Puzosia mayoriana
Desmoceras parandieri, etc. paronae
Desmoceras beudanti
latidorsatum
Douvilleiceras mamillatum
Turrilites gresslyi
JJ. E. Fallot: fitude geologique sur les etages moyens et superieurs du terrain
cretace dans le Sud-Est de la France. Ann. des Sciences geol., 1, 268 p., 41 fig., 8 pi.,
1885.
2J. Blayac: Le Gault et le Cenomanien du bassin de la Seybouse et des hautes
plaines limitrophes (Algerie) C. R. Acad. Sci., CXLIII, 252-5, 1906.
66 University of Texas Bulletin
ALBIAN
In the province of Algiers, near Aumale, Peron1 found marls with ferruginous fossils:
Natica Phylloceras velledae
Solarium Pozosia mayoriana
Cerithium Desmoceras latidorsatum
Nucula Desmoceras beudanti
Leda Uhligella dupiniana
Astarte
CENOMANIAN
The Cenomanian is uniformally represented in Northern Tunis by an alternation,
indefinitely repeated, of marls and limestones. According to Pervinquiere,2 only the
lower part of the stage is fossiliferous. Here a Vraconian fauna is found, with the
following species preserved as ferruginous molds:
Phylloceras ellipticum? Kossmat Turrilites Bergeri Brongniart
— Velledae Mich. var. Seresitensis — Wiesti? Sharpe
Pervinquiere — Morrisi Sharpe
— Tanit Pervinquiere — Scheuchzerianus Bosc.
— decipiens Kossmat — costatus Lamarck
Lytoceras Flicki Pervinquiere — Puzosianus d'Orbigny
cf. Marut Stoliczka — Kerimensis Pervinquiere
— Timotheaum Mayor Forbesiceras obtectum Sharpe
— cf. Kingianum Kossmat Saynoceras Gazellae Pervinquiere
Hamites simplex d'Orbigny Scaphites aequalis Sowerby
— virgulatus Brongniart — obliquus Sowerby
— armatus Sowerby — Thomasi Pervinquiere
Baculites baculoides Mantell Puzosia Paronae Kilian
Puzosia Chirchensis Pervinquiere Mortoniceras Nicaisei Coquand
— Mayoriana d'Orbigny — proratum Coquand
Placenticeras Uhligi Choffat Tunesites Salambo Pervinquiere
— Saadense Th. et. P. Acanthoceras Brottianum d'Orbigny
Flickia simplex Pervinquiere — Martimpreyi Coquand
Brancoceras Zrissense Pervinquiere — Aumalense Coquand
Mortoniceras inflatum Sowerby with its var, — Suzannae Pervinquiere
subinflata, spinosa and orientalis Stoliczkaia dispar d'Orbigny
Belemites (Hibolites) minimus Lister
Pervinquiere3 has described many Cenomanian ammonites from Algeria, some of them
ferruginous; the fauna contains Phylloceras, Lytoceras, Hamites, Scaphites, Puzosia,
Acanthoceras, Turrilites, Mortoniceras, and several other common genera, and is sim-
ilar to that of Tunis.
1A. Peron: Essai d'um description geologique d'Algerie pour servir de guide aux
geologues dans 1'Afrique franchise. Ann. des Sci. Geol., xiv, art. 4, 202 pp., figs. 1883.
2Pervinquiere : Et. pal. tun., Cephalopodes, pp. 417-418.
3Pervinquiere, Sur quelques ammonites du cretace algerian. Mem. Soc. Geol. France,
No. 42, 1910.
Weno and Pawpaw Formations
67
Boule, Lemoine and Thevenin1 cite from Madagascar a series of sandy
clays of middle and upper Cenomanian age, containing pyritic fossils.
These clays are characterized by Acanthoceras subvicinale B. L. & T.,
Scaphites aequalis Sowerby, Belemnites fibula Forbes, Ostrea foisseyi
Lemoine, and contain Acanthoceras prenodosoides B. L. & T., Phylloceras
forbesianum d'Orbigny, P. diegoi B. L. & T., etc.
PARALLELS BETWEEN WENO-PAWPAW FOSSILS AND FOSSILS OF THE
EUROPEAN AND AFRICAN CENOMANIAN AND VRACONIAN
*H.
*T.
Texas
*Scaphites hilli Adkins and*S.
Winton
•Flickia boesei Adkins *F.
*Acanthoceras worthense *A.
Adkins
•Acanthoceras sp. *A.
*Hamitestenawa Adkins and *H.
Winton
•Hamites sp.
*Turrilites worthensis
Adkins and Winton
*Baculites comanchensis
Adkins
*Mortoniceras worthense
Adkins
*Puzosia sp.
*Lytoceras sp.
*Metopaster hortensae
Adkins and Winton
*Comptonia- wintoni Adkin
Schloenbachia wintoni
Adkins
Corbula Wenoensis Adkin.'
Pinna guadalupae Bose
Pecten texanus Roemer
Pecten subalpinus Bose
Plicatula subgurgitis
Bose
Ostrea carinata ?
Lamarck
Ostrea marcoui Bose
Gryphea washitaensis
Hill
Africa (Tunis)
aequalis Sowerby
Europe
S. aequalis Sowerby
simplex Pervinquiere
martimpreyi Coquand A.
suzannae Pervinquiere
simplex d'Orbigny H.
armatus Sowerby
wiesti Sharpe
martimpreyi Coquand
simplex d'Orbigny
H. armatus Sowerby
B. baculoides Mantell
B. baculoides Mantell
*M.
*P.
L.
inflatum var. spinpsum
Pervinquiere
paronae Kilian
marut Stoliczka
M. parkinsoni Forbes
C. comptoni Forbes
S. rostrata
C. bicarinata Noetling
P. decussata Goldfuss
P. alpinus d'Orbigny
P. alpinus d'Orbigny
P. gurgitis Pictet
O. carinata Lamarck and
O. frons
O. syphax Coquand
G. vesiculosa Sowerby
'Boule, Lemoine and Thevenin, Paleontologie de Madagascar, Cephalopodes cretaces
des Environs de Diego-Suarez, Ann. de Pal., vol. 1, fasc. 4, pp. 2, 4, 1906.
68
University of Texas Bulletin
Helicocryptus mexicanus
Bose
Holectypus limitis Bose
Enallaster bravoensis Bosc
Epiaster aguilerae Bose
Hemiaster calvini Clark
H. radiatus Sowerby
H. cenomanensis Gueranger
E. lepidus de Loriol
E. triangularis d'Orbigny
H. latigrunda Peron and
Gauthier
DESCRIPTION OF SPECIES'
CEPHALOPODA
NAUTILUS TEXANUS Shumard
i860: Nautilus texanus Shumard, Trans. Acad. Sci., St. Louis, 1, 1856-60.
1889: Nautilus texanus Hill, Geol. Surv. Texas, Bull. 4, p. 21.
1893: Nautilus texanus Cragin, Geol. Surv. Texas, 4th Ann. Kept., p. 236.
1895: Nautilus washitanus Cragin, Colo. Coll. Stud., 5, p. 67.
1902: Nautilus texanus Shattuck, U. S. G. S., Bull. 205, p. 34, pi. XXIII, figs. 1-2,
pi. XXIV, figs. 1-2.
1920: Nautilus texanus Adkins and Winton, Univ. Texas Bull. 1945, p. 32, pi. 20,
figs. 1-2.
1920: Nautilus texanus Winton and Adkins, Univ. Texas Bull. 1931, pp. 58, 61, 66.
This is the commonest Cdmanchean Nautilus, and has a known range
from the basal Duck Creek limestone (at Denison, Texas) to the Buda
limestone (at Austin, Texas). It has a zone of abundance in the top of
the Weno limestone, and one in the top of the Fort Worth limestone.
NAUTILUS sp.
The upper Pawpaw clay contains considerable numbers of small Nautili
of a size about one-third that of Nautilus texanus Shumard. These Nau-
tili are more closely coiled, have a smaller umbilicus, a much thicker and
lower volution, and apparently are smooth. The species is not described
here because of the poor preservation of the material at hand.
1Types and figured material are deposited in the Bureau of Economic Geology,
Austin, unless otherwise specified in the text. The types at Austin are in a metal
locker in the fireproof vault of the University of Texas Library. Most of the photo-
graphs were made by Mr. F. Christiansen, Austin, but for some I am indebted to
Professor John Davis, Fort Worth.
Weno and Pawpaw Formations 6i)
AMMONITES1
HAMITES TENAWA Adkins and Winton
1920: Hamites tenawa Adkins and Winton, Univ. Texas Bull. 1945, p. 43, pi. 6, fig. 4.
1920: Hamites tenawa Winton and Adkins, Univ. Texas Bull. 1931, p. 21.
1920: Hamites sp., Winton and Adkins, ibid., p. 69.
HORIZON: Pawpaw formation, clay fades, base.
LOCALITY : About three miles southeast of Haslet, Tarrant County,
Texas (type locality); 714, near Fort Worth, Texas; 723, Glen Garden
Country Club, near Fort Worth, Texas.
Among several Hamites in the Pawpaw clay is a straight equal ribbed
species resembling Hamites simplex. The species and its suture have
been figured elsewhere; the suture has six lobes and six saddles, mainly
bifid and slightly dissected.
HAMITES sp. aff. ARMATUS Sowerby
HORIZON: Base of the Pawpaw formation, clay facies.
LOCALITY : 714, near Fort Worth, Texas.
Fragments of a small Hamites preserved in hematite and showing on
every second or third rib lour tubercles, two lateral and two ventral, are
found in the basal third of the Pawpaw clay. The suture is rather similai
to that of Hamites armatus Sowerby and has the following characteris-
tics : Suture consists on each side of three saddles and two lobes, in ad-
dition to the siphonal and antisiphonal lobes ; suture much more dissected
than that of Hamites tenawa; siphonal saddle narrow and low, with three;
rounded subdivisions; siphonal lobe narrow, bifid, each lobule narrow at
base, trifid terminally; first lateral saddle longer and much broader than
siphonal lobe, flared terminally, bifid, each division twice bifid and laterally
'In coiled ammonites the external margin of the volution (often keeled) is ventral
and the internal, concealed margin is dorsal; the sides of the volution are the flanks,
the terminal opening is the aperture. Lobes point backwards, away from the aperture,
and saddles forwards, toward the aperture. The siphonal (external, ventral) lobe lies
on the ventral mid-line and its angulated lobules point backwards; the antisiphonal
lobe lies on the dorsal mid-line and its lobules point backwards. Next to the siphonal
lobe and on each side of it is the first lateral saddle, and dorsal to it the first lateral
lobe ; still more dorsally the second lateral saddle, then the* second lateral lobe. Further
saddles and lobes are numbered seriatim and are often called adventitive elements.
In straight shells (Hamites, Baculites, Ptychoceras, straight portions of Scaphites)
and in fragments of Turrilites, the siphuncle should first be located; the siphonal lobe
lies upon it.
70 University of Texas Bulletin
dissected; first lateral lobe narrow, laterally dissected, twice bifid term-
inally; second lateral saddle slightly broader, twice bifid; second lateral
lobe lower, simpler, bifid, dissected laterally; third lateral saddle low,
broad, rather simple, twice bifid; antisiphonal lobe very simple, rounded,
slightly trifid at tip, nearly twice as tall as broad.
ANCYCLOCERAS BENDIREI n. tp.
PL 11, fig. 1
1920: Hamites sp. B. Winton and Adkins, Univ. Texas Bull. 1931, p. 22.
MEASUREMENTS: Diameter of shell without tubercles, dorsoven-
tral, at small end of fragment 19 mm., at middle of curve, 28 mm., at
large end of curve 25 mm. ; same diameters, right-left, respectively, 16.5
mm., 22 mm., 24.5 mm. Number of ribs in 5 cm. along straight portion,
7; on curve, 4; average number of dorsal costellae per centimeter, 6.
HORIZON: Base of Weno formation, marl facies.
LOCALITY : 618 (type locality) , middle exposure, about 10 feet above
the top of the Denton marl, near Fort Worth, Texas. The type, consist-
ing of three fragments, and a fragment of another individual were found
here.
DESCRIPTION : Two limbs connected by a curve ; of these a greater
part of the thicker limb and a part of the thinner limb are missing. There
is not enough of the curve present to detect a spiral winding of the
coil. The smaller, ascending limb increases moderately in diameter to
the curve, where the fragment has its greatest thickness. There are
four symmetrically placed rows of prominent, rather slender spines, two
ventro-lateral and two mid-lateral. The spines of the two ventro-lateral
rows are coarser and are laterally flattened at the base ; those of the mid-
lateral rows are more slender and are circular at the base. These spines
are widely spaced, and a set of the four spines lies on each rib. The ribs
are coarse, remote, and in a plane nearly at right angles to the long axis,
however, they slant ventrally towards the aperture, and dorsally from the
last line of tubercles are continued as obscure elevations which cross the
dorsum as narrow, fine ribs. The four rows of tubercles bound three
flat longitudinal strips, one mid- ventral and two ventro-lateral; the re-
mainder of the circumference is evenly curved. The cross section of the
shell is therefore hexagonal in its ventral half and short oval in its dorsal
half. Shell and suture are preserved.
Weno and Pawpaw Formations
71
SUTURE : Similar to that of Ancycloceras lineatus Gabb1 and Hamitet
quadrinodosus Jimbo.- Suture consists of medium sized siphonal lobe
small antisiphonal lobe, and large, nearly equal, first and second lateral
lobes and first and second lateral saddles ; the third lateral saddle is smaller.
Details of siphonal lobe indistinct; the next four elements are large,
slender, spreading, subequal, much dissected, primarily bifid, the subdivi-
Fig. 2. Ancycloceras bendirei n. sp., suture of the type individual, camera lucida
drawing, x 5. SL — Siphonal lobe; ASL — Antisiphonal lobe.
sions bifid, and the resulting inflections generally minutely trifid, some-
times bifid, at the tips. These four elements are subquadrate and sub-
equal. The third lateral saddle is smaller, laterally dissected and twice
bifid terminally. The antisiphonal lobe is about twice as tall as wide,
laterally dissected, and trifid terminally, the central prolongation being
the longest.
This species is not closely similar to any known to me. It has some-
what the form of Hamites obstrictus Jimbo, but differs in having four
rows of prominent slender spines, and in the ribs, which are coarser and
more widely spaced. Superficially also it resembles in form Ancycloceras
matheronianum d'Orbigny (Neocomian), but differs from this species in
the suture, especially in the size of the siphonal lobe and the amount of
dissection of the lateral elements, in the diminished lateral ribs and in
the presence of spines throughout the length of the coil instead of tubercles.
HAMULINA WORTHENSIS n. .p.
PI. 2, figs. 23-26
This fossil has two non-contiguous straight limbs united by a single
curve, and furthermore the suture has six lobes in all, like Hamulina hamus
'Gabb, Geol. Snrv. Calif., Paleontology, vol. 2. p. 139, pi. xxiii, fig. 18c.
o, Pal. Abh., vi, 3, 1894.
72 University of Texas Bulletin
(Quenstedt) and H. quenstedti Uhlig.1 The juvenile portion of the shell,
absent in the material at hand, may have been a close coil as in Macro-
svaphites, as indicated by the grooved impression on the long limb, but this
is not certain, and in addition the suture forbids identification with Macro-
scaphites. The suture and the absence of ribbing prevent its reference to
Ancycloceras. Bose2 describes a similar Hamulina sp. from the Vraconian
limestone blocks of Camacho, Zacatecas.
MEASUREMENTS :
I (type) II III IV
Length of fragment 7.8 mm. 10.0 8.9 8.1
Width, lower end 1.6 1.0 1.5 1.7
Width on bend 3.0 2.1 2.2
HORIZON : Base of the Pawpaw formation, clay facies.
LOCALITY : 714, near Fort Worth, Texas. The type and two other
individuals have been found here.
Three fragments of a straight limbed ammonite, all lacking the aper-
ture and part of the larger limb, were found in the basal Pawpaw clay.
In the absence of better material their systematic position can not be set-
tled, and I assign them with hesitation to the genus Hamulina. The
curve connecting the larger limb is preserved, but this limb made no im-
pression on the inner face of the smaller limb, as in some Ptychoceras,
and therefore was not in close contact with it; in addition, the visible
portion of the curve is open, indicating a distant, possibly short, thick
limb. This might suggest Hamulina or Ancycloceras, which mostly differ
in their sutures and their prominent ribbing. Whether there were three
limbs as in Diptychoceras, is unknown ; however, the suture is very differ-
ent from, and less dissected than that figured by Gabb for his Diptycho-
ceras laevis (laeve)3 and that species also differs greatly in form from
ours.
Two other individuals (Plate 2, figures 23-25) show distinctly the curve
and the proximal portion of the shorter, thicker limb. This is free, and
is separated from the thinner limb by the space of about half of its
thickness. The aperture is not visible. One individual (Plate 2, figures
23, 25) shows also a part of the curve at the lower end of the slender
limb. This end turns with about the same curvature as that of the larger
curve, and on the venter of the lower end of the slender limb is a wedge-
iPervinquiere, fit. pal. tun., Ceph., pp. 88-89.
2B6se, On some new Cretaceous Faunas from Mexico, Univ. Texas Bull, (in p'ress).
"Gabb, Pal. Cal., II, pp. 142-5, pi. xxv, fig. 21a-b.
ana fa^^Kiw Formations 73
shaped groove about 1 mm. long with the shallowing, pointed end towards
the aperture, which indicates that the lower end of this ammonite was a
close coil, as in Ancycloceras, or a closely apposed limb. These three
individuals agree essentially in their sutures.
DESCRIPTION: Only fragments preserved, showing a small limb,
the curve connecting with the larger limb, and a portion of this limb.
Suture present ; shell, aperture and lower portion of slender limb absent.
The curve, in the type individual does not quite turn to a position parallel
to the small limb; and the two limbs are not in contact, at least at the
curve. Dorsal side with a central and two lateral flattened smooth strips
(the antisiphonal lobe lies on the former), making the cross-section near
the turn a very thick crescentic or kidney bean shape, slightly concave
dorsally and broadly convex ventrally. The smaller limb is slender in
its younger stages and thicker to a point near the curve; here there is a
slight dorsal inflation beyond which are no sutures; farther up, at the
curve, there is a slight dorsal constriction. The ventral mid-line bears
a small ridge which apparently marks the siphuncle.
SUTURE : The suture is but slightly dissected, and consists of two
Fig. 3. Hamulina worthensis n. sp., Sutures of type individual, camera lucida drawing,
x 16.
lateral lobes and three saddles, in addition to the siphonal and1 anti-
siphonal lobes. The siphonal lobe is bifid and has two slender elongate
tips ; it is about twice as tall as broad. The first and second lateral saddles
are nearly equal and similar; each is about half as tall as broad, and is
bifid by a shallow, simple lobule. The first lateral lobe is trifid and pro-
gressively diminishes in size from the younger to the older sutures. The
second lateral lobe is rather smaller than the first, and is bifid. The third
lateral saddle is of the same height and about half the width of the other
two, and is broadly rounded and unequally bifurcated by an angular notch
74 University of Texas Bulletin
lying nearer the antisiphonal lobe and making the more dorsal division
smaller than the more lateral one. The antisiphonal lobe is peculiarly
narrow and elongated, and has a slightly inflated, bifid tip.
The suture has the same number of elements, six lobes and six saddles,
as Ptychoceras, and the species seems to have some resemblance to
P. laeve, var. hamaimensis Pervinquiere1 (Lower Gault, Tunis) ; however,
the first two saddles of our species are broader and less dissected; the
third saddle is unequally and shallowly bifid ; the first lateral lobe is
trifid instead of bifid ; and the other lobes are bifid. The African species
also differs greatly in form from ours, in having two apposed limbs and
annular constriction and inflations on the thicker limb. The Texas Upper
Cretaceous (Navarro) species Ptychoceras texanum (Shumard)2 has the
two limbs strongly ribbed and closely apposed.
BACULITES COMANCHENSIS n. sp.
PI. 2, figs. 20-22
1920: Baculites sp., Winton and Adkins, Univ. Texas Bull. 1931, pp. 21, 69.
MEASUREMENTS :
I (type) II III
Length 12.5 17.3 13.4
Smaller end, major diameter 3.3 4.0 3.9
Smaller end, minor diameter 2.9 3.4 3.0
Number of ribs in 5 mm 5 1-2
Larger end, major diameter 6.1
Larger end, minor diameter 3.4 3.7 3.1
Number of ribs in 5 mm 4 1-2 3
A characteristic Pawpaw baculite lacking the aperture and the coiled
portion, will be described here on account of its stratigraphic importance.
The straight portion is preserved with the sutures, as a limonite cast.
HORIZON : Pawpaw formation, clay facies, base, rare.
LOCALITIES: Individual II from locality 714, near Fort Worth,
Texas; type individual (PL 2, fig. 21) and the others from locality 719,
west — facing hill to east of Crowley road, one! mile south of the Baptist
Seminary, four and a half miles south of Fort Worth, Texas.
DESCRIPTION: Straight fragments preserved, slightly and uni-
formally tapering, lateral outlines slightly undulating but on the whole
straight; cross-section a short oval; living chamber not preserved, but
'Et. pal. tun., p. 90, pi. IV, figs. 5, 6a-b.
c. Bost. Soc. Nat. Hist., 8, 1861 (1862), p. 190.
Weno and Pawpaw Formations 75
sutures suddenly more crowded at larger end. Ribs consist of evenly
rounded, low, annular swellings in a plane nearly perpendicular to the
long axis of the shell, more crowded near the enlarged end, almost equally
steep on both sides of the annulation, tallest on the venter and on the
ventral half of the sides, thence decreasing in height toward the dorsum,
where they turn sharply toward the more constricted end of the shell
and become obsolete upon crossing the dorsum. Over the more constricted
lower end of the shell a suture lies in the lower half of the valley between
each two annulations, but in the thicker part of the shell the relation of
sutures to annulations is variable; near the thicker end in the type, the
sutures are crowded.
SUTURE: Besides the siphonal and antisiphonal lobes, the sutural
elements consist of three lateral saddles and two lateral lobes. The
Fig. 4. Baculites comanchensis n. sp., sutures of type individual, camera lucida draw-
ing, x 8.
siphonal lobe is bifid, having two slender, rather acute points and a rela-
tively broad, low, crenulate, external saddle; this lobe is nearly twice as
tall as broad. The antisiphonal lobe is extremely small and simple; it
consists of a single long, narrow, rounded point. The first lateral saddle
is about twice as wide as the siphonal lobe and is deeply bifid by a rather
simple lobule with one central and two incipient lateral points; each of
these portions is again bifid. The first lateral lobe is very tall and bi-
furcated terminally.1 The second saddle is bifid and not quite as wide
as the first; of its divisions the ventral one is trifid and the dorsal one
bifid. The second lobe is broader at the base than the first, and about
two-thirds the height; it is bifid terminally. The third saddle is broadly
rounded and shallowly bifid. The suture (Fig. 5) is peculiarly simplified
and is very characteristic. It is somewhat similar to that of Baculitef,
vertebralis Lamarck (Santonian), but differs in having a very simple and
reduced antisiphonal lobe and third lateral saddle, and in the greater
breadth and simplicity of its first and second saddles. It has even less
resemblance to Baculites baculoides Mantell (Vraconian), whose saddle?
'If the lobes are trifid the fossil belongs to Bochianites Lory; however, the suture
agrees better with Baculites.
7li University of Texas Bulletin
and lobes are narrow, much dissected and constricted basally. I have not
had opportunity to compare this species with other Vraconian and Albiar,
species.
TURRILITES BOSQUENSIS n. sp.
PL 3, figs. 3, 7
MEASUREMENTS :
Height of spire 21 mm.
Diameter of last volution . 12 mm.
Aperture, height 7.2 mm.
Aperture, breadth 6.1 mm.
HORIZON: Middle of Del Rio clay at top of abundant horizon of
Exogyra arietina Roemer, in association with Flickia 1 bosquensis Adkins,
Acanthoceras worthense Adkins, Pecten subalpinus (Bose), Gryphea
mucronata Gabb, and small pyrite fossils. The turrilite apparently is
abundant.
LOCALITY : West bank of the South Bosque River, 150 yards south
of the bridge on the Speegleville road, tall Del Rio cliff, 5.5 miles west of
the courthouse at Waco, Texas (type locality) .
DESCRIPTION: Shell conical, sharp spired, spiral angle 37 degrees
near tip but spreading slightly on the last volution, sinistral, turreted,
five volutions in the type, decreasing rapidly in size towards the apex.
In side view the volutions are more angulated and the tubercles relatively
more prominent than in any other known Texas turrilite. There are
four spiral rows of tubercles, of which three are large and nearly equal
and lie on the prominent flank of the volution and the fourth is diminu-
tive and lies beneath the upper margin of the volution. The third row
of tubercles lies at the exact margin between the volutions and is there-
fore covered as is the fourth small row, by the succeeding volution, so that
on the earlier volutions only two rows of tubercles are exposed. Of these
the lower row, nearest the siphuncle, is separated from the lower ex-
posed margin of the volution by a broad smooth evenly curved spiral
strip.
Tubercles of the first and second rows1 are obliquely placed and are
not connected by visible ridges. The third row is closely spaced, the
tubercles being more numerous than in the first two rows, and this row
1Counting from below when the turrilite is placed point down (See Pervinquiere,
Et. pal. tun., Ceph., p. 428). The siphuncle is then inferior and may be concealed
by overlap of the next volution.
Weno and Pawpaw Formations 77
is separated from the second row by a sharply excavated spiral groove
of only half the width of the space separating the first two rows. Finally,
the small tubercles of the fourth row are paired with the tubercles of
the third row, the tubercles of a pair being connected by an obsolete radial
ridge.
The angularity of the volutions is caused by the lateral projection of
the first and second rows of tubercles. In the type individual, the sec-
tion of the last volution (pi. 3, fig. 7) is elliptical in its basal (dorsal)
half, and the inner margin is evenly rounded. The superolateral margin
is incised between the three prominent tubercles, and the superior margin
in the region of the fourth line of small tubercles is almost straight.
SUTURE: The type individual shows a series of suture stages be-
ginning on the earliest preserved volution. This volution is rounded and
I .•»*•• o/ Q
1 o20, °*
Fig. 5. Turrilites bosquensis n. sp., sutures of type individual, camera lucida draw-
ing, x 8. The numbers indicate the volutions on which the corresponding
sutures occur.
is totally smooth and tubercles begin to appear only at a diameter of
spiral of 2.8 mm. At this point the volution is 1.1 mm. thick and the
first and second rows of tubercles appear simultaneously. The suture
is simple and consists of a low, undissected siphonal lobe, a simple first
lateral saddle, a slightly smaHer and still undissected first lateral lobe,
a slightly bifid but otherwise simple second saddle, and an undivided
78 University of Texas Bulletin
second lateral lobe, of which half is concealed by the next volution. The
siphonal lobe of the second volution is dissected, and the two lateral sad-
dles are bifid with simple rounded subdivisions, but the lateral lobes are
rounded and undivided. On the third volution the saddles become still
more complicated, in general being trifid, but the lateral lobes have little
inflection. The siphonal lobe has elongated to its final form but still
lacks secondary inflections. In the fourth volution the siphonal lobe is
subdivided laterally, and has mature inflections and form. The lateral
lobes are slender and trifid, and the lateral saddles are dissected, in general
twice trifid. The final volution of the type individual has all elements
of the suture dissected (the siphonal lobe was poorly preserved and likely
is more dissected than is shown in the drawing) . The first saddle is twice
as broad as the first lobe and is broadly bifid. The second saddle is bifid
and the second lobe in this individual indeterminate.
Number of individuals: about 10.
TURRILITES WORTHENSIS Adkins and Winton
PI. 3, figs. 1, 6
This common Pawpaw species marks the clay phase in the region from
Denton to Johnson County, Texas. It is more abundant in the basal five
feet of the formation. The species is rare in the marl transition phase,
one individual having been found near Riovista. The species is very
rare or missing in the Red River region.
TURRILITES sp.
PI. 3, figs. 2, 4
There are several dextral and sinistral turrilites, preserved in hematite
or pyrite, which characterize the Pawpaw clay, and material is being
collected for a further study of their structure. In numbers these tur-
rilites are abundant and are one of the most striking features of the
fauna. They likewise are rare except in the clay facies, and have not
been found so far, north of Denton County or south of Johnson County,
Texas. Turrilites similar to these species have been found in the Del
Rio clay just above the Exogyra arietina horizon (equivalent of Grayson
formation) near Waco and Austin, Texas.
Weno and Pawpaw Formations 79
SCAPHITES HILLI Adkins and Winton
PI. 2, figs. 1-12
1920: Scaphites hilli Adkins and Winton, Univ Texas Bull. 1945, p. 37, pi. 7, figs. 3-6.
1920: Scaphites hilli Winton and Adkins, Univ. Texas Bull. 1931, p. 21.
1920: Scaphites sp. A. Winton and Adkins, ibid., pp. 21, 69.
I II III IV V VI
PI. 2, PI. 2, PI. 2, PI. 2, PI. 2, PI. 2,
Fig. 1 Fig. 4 Fig. 7 Fig. 8 Fig. 12 Fig. 17
MEASUREMENTS
Greatest length 9.6 9.5 13.5 11.0 8.0 7.5
Greatest thickness 8.2 4.4 7.3 4.8 7.0 6.5
Diameter of coil 7.8 3.8 6.0 6.5 7.0 6.2
Length of uncoiled portion .... 5.0 8.0 7.5 .... ...:
Thickness of last turn 8.2 4.4 4.5 2.6 2.6 3.6
Thickness of next to last turn 3.6 3.1 1.5-
Greatest length of umbilicus 1.8 1.2 2.1 2.0 1.6 1.2
Number of (ventral) ribs per
centimeter, on coil 20 28 20 26 32 26
On uncoiled portion 24 26 .30
HORIZON: Basal half of Pawpaw formation, clay phase. This
species has so far not been found outside of Tarrant County, Texas, but
it may be expected throughout the extent of the clay phase of the Pawpaw,
or farther.
LOCALITY: Most frequent at the type locality one-fourth mile south
of the International and Great Northern Railway bridge across Sycamore
Creek, Fort Worth, Texas (locality 714), and one-half mile west of the
Glen Garden Country Club, Fort Worth, Texas (locality 723).
NUMBER OF INDIVIDUALS : About 25 individuals have been found.
These are in the Bureau of Economic Geology, Austin, Texas, and Texas
Christian University, Fort Worth, Texas.
TYPE INDIVIDUAL: From locality 714 (described above) : deposited
in Walker Museum, Chicago.
MODE OF PRESERVATION: Type, dark reddish brown hematite;
other individuals light reddish yellow limonite; a few scattered pyrite
cubes noted.
DESCRIPTION: This scaphite consists of a coiled portion and an
elongate unrolled portion terminating in the aperture, and at their junc-
tion there is a prominent dorso-lateral tubercle or geniculation which may
be taken as an orienting point in describing the ribs and sutures of this
fossil.
80 University of Texas Bulletin
The coiled portion consists of an unknown number (3 or 4 ?) volutions,
and the umbilicus is deep and, due to the position of the dorso-lateral
tubercle, has a kidney-bean shape with the end nearer the aperture some-
what pointed. There is a distinct elongation, which in the absence of
the uncoiled portion will orient the shell.
For the most part there are no sutures nearer the aperture than the
dorso-lateral tubercle, and the uncoiled portion represents the living
chamber, and therefore lacks sutures.
Coiled portion ventricose to subglobular, very obese, subovate in out-
line, evenly and almost circularly rounded ventrally ; dorsally the circular
margin is broken by the incurved margin of the dorso-lateral tubercle,
resulting in a more or less open crescentic or tear-shaped umbilicus, lying
slightly oblique to the axis of the uncoiled portion; greatest transverse
diameter of coil ventral to this tubercle; coil slightly constricted just above
the tubercle. The uncoiled portion of which the part below the tubercle
is the living chamber, is elongate and ornamented with numerous fine
ribs which course obliquely from the dorso-lateral margins to the venter,
being nearer the aperture at the latter point. The living chamber is in-
flated at the edges at the dorso-lateral tubercle where it is in contact,
with the coil, constricted dorsally at a point a little nearer the aperture
and thereafter on approaching the aperture is constricted and curved
dorsally. Its dorsal side is excavated into a prominent groove, whose
width is about half that of the living chamber, and into which the coil
fits at the upper end; the groove thus is exposed from the coil to the
aperture. The resulting cross section of the living chamber is concave-
convex, the short dorsal concave margin passing over the sharply rounded
edges of the dorsal groove into the longer lateral and ventral margin.
This section varies at different points of the scaphite; near the aperture
it is more concave dorsally.
FORM : There is a variation in form, amount of embracing and rate
of increase in size of the successive volutions, as is seen also in the inter-
grades between Scaphites obliquus and Scaphites aequalis.1
The type of Scaphites hilli is an obese individual with thick, rapidly
expanding volutions, which closely approaches the typical S. aequalis
Sowerby as figured by Pervinquiere. This expansion over the last volu-
tion of the coil amounts to a doubling of the breadth of the coil, the
breadths at the dorso-lateral tubercle and at the point opposite it on the
next volution being in the ratio of 8:3.6 in the type. The amount of
thickening interiorly is also great, since the umbilicus is deep. The re-
'Pervinquiere, Et Pal. Tun., pp. 118-120.
Weno and Pawpaw Formations 81
suiting cross-section of the last turn is thickly crescentic (pi. 2, fig. 1).
The remaining individuals have thick coils but show a less rapid ex-
pansion of the last volution. One individual (pi. 2, fig. 7) has preserved
most of the uncoiled portion which is a thick crescent with rounded sides
and a relatively narrow non-ornamented dorsal groove; the aperture is
destroyed. Usually only the coiled portion is preserved, and these in-
dividuals are of variable size, even when the dorso-lateral tubercle is also
present. They have the same relative thickness and expansion of the coil
as the individuals of S. aequalis figured by Pervinquiere.1 It is notable
that the ribbing becomes obsolete over the lower half of the dorso-lateral
tubercle and the entire apertural region.
A straight groove of variable prominence along the ventral midline is
a feature of all material found.
RIBS : The ribs are branched or unbranched. They are most numer-
ous at the ventral mid-line and thence laterally some stop short of the
dorso-lateral margin and some pass over this margin with a pronounced
sigmoidal flexure and describe across the dorsum an arcuate curve, con-
vexed towards the aperture. These principal ribs are thick and elevated
laterally. In addition there are shorter ribs which are best developed
at the venter and disappear at both ends, or else branch from a principal
rib laterally, and crossing the venter disappear laterally, on the opposite
side of the coil. There is some irregularity in the distribution of these
types of ribs, as follows: In one invividual (pi. 2, fig. 7) in the region
at the end of the uncoiled portion there are long and short simple ribs
and branched ribs but the long simple ribs predominate. In the branched
ribs the point of branching is far ventral, lying one-third the distance from
the ventral midline to the dorsal midline. Near the dorso-lateral tubercle
there are long and short simple ribs with rare incipient branching; the
short ribs decrease in length, as their ends lie farther from the umbilicus.
The same statements hold for the other individuals figured. In the distal
half of the outer volution of the coiled portion a short simple rib alter-
nates with a -long simple rib ; however, there is incipient branching in the
long ribs opposite the dorso-lateral tubercle (pi. 2, fig. 7) sporadically
near the tubercle (pi. 2, fig. 4) or even over the whole distal half of the
volution (pi. 2, fig. 12). In one individual (pi. 2, fig. 8) there are alter-
nate long and short simple ribs next to the tubercle, but more proximally,
there is an irregular alternation of simple and branched ribs. In general,
this region shows an alternation of long simple ribs with short simple,
ones, and incipient or developed branching. This is the situation in the
'Et. Pal. Tun., plate IV, figures 24-26.
82
University of Texas Bulletin
type individual (pi. 2, fig. 1) in which the ribs are at some places evi-
dently branching, and at other places apparently of alternate length.
The remaining visible portion of the coil shows in general an alter-
nation of one branched with one unbranched rib. This alternation is
often irregular ; in pi. 2, fig. 8 the simple ribs preponderate. The branch-
Jng may be incipient giving the impression of an alternation of one
branched rib with two simple ribs or of one long simple rib alternating
with two short simple ribs (pi. 2, fig. 12) . In one individual (pi. 2, fig. 12)
a branch from a principal rib at one umbilical margin crosses the venter
and fuses with the next principal rib, giving a zig-zag ribbing.
Briefly the ribbing is more branched on the coil and simpler' on the
straight portion. It is seen that the ornamentation of the coil somewhat
resembles that of S. meslei Grossouvre (Coniacian), which, however, has
the principal ribs more prominent and the secondary ribs largely un-
branched; this species also unrolls much less rapidly than the type of
S. hilli. The obesity of the typical S. hilli also removes it from S. obliquus
as does the coarseness of its ribbing; in fact, no individual known ap-
proaches S. obliquiis in either respect. In both respects it is similar to
the thick coiled examples of S. aequulis Sowerby, from which it differs
in the rate of increase of its turns, in the dorso-lateral tubercle and shape
of the umbilicus, and in the suture. S. aequalis shows the same prom-
inence of the primary ribs near the umbilical margin and the same branch-
ing laterally on the coil, as S. hilli.
Fig. 6. Scaphites hilli Adkins and Winton, suture, type individual, camera lucida
drawing, x 12. The fossil is figured on PI. 2, fig. 1.
SUTURE: Figure 6 shows the suture of the type, so far as can be
seen without dismembering the scaphite. This well developed suture has
externally besides the siphonal lobe, two conspicuous lobes and near the
umbilical wall a third irregular, low, wide lobe. Of these, the first lateral
Weno and Pawpaw Formations 83
lobe is narrow, very tall, and trifid, with the central point strongly de-
veloped. The second lateral lobe is broad, nearly the same height as the
siphonal lobe, its breadth being about six tenths that of the first saddle,
and is bifid with each lobule split into rounded tips. The third lobe is
twice as broad as tall and is obscurely split into four rounded divisions.
The first saddle is large, subquadrate in outline and deeply bifid; each
division is split by a lobule into two unequal bifid components. The second
saddle is bifid. The third saddle, which lies on the umbilical wall, is
wide and low.
Fig. 7. Scaphites hilli Adkins and Winton, young individual, showing the last five
sutures, camera lucida drawing, x 10. The fossil is figured on PL 2, figs. 3-4.
A comparison of the mature suture of the type with juvenile suture
stages is represented in figure 7. This individual differs from the type
in many ways ; it is less obese and its coils increase less rapidly ; its rib-
bing is possibly coarser; its first lateral saddle is shallow and very wide
and is split by a shallow lobule, whereas it is tall, narrow and split by a
deep lobule in the type of S. hilli; the two have the same horizon and
range and are apparently connected by intergrades. The situation is
somewhat similar to that of Scaphites aequalis and S. obliquus, and until
further material is available, I would refer this form to S. hitti. This
suture is seen to be simpler and to lack the finer divisions of saddles and
lobes seen in figure 6. The lobes on both individuals are, however, bifid.
84 University of Texas Bulletin
The internal suture of a small individual whose form and ribbing mainly
agree with the last named individual is shown in figure 8. This suture
has six lateral and internal saddles and five lobes. The anti-siphonal lobe
is trifid, the remaining ones bifid.
AT^
Fig. 8. Scaphites hilli Adkins and Winton, external and internal suture, camera
lucida drawing, x 10.
Very closely related to this species is Scaphites worthensis Adkins and
Winton (Duck Creek marl) which, however, lacks the ventro-lateral tu-
bercle; its suture also differs in several respects. Scaphites semicostatus
Roemer and S. texanus Roemer, have been described from the Eagleford
formation near New Braunfels; S. vermiculus Shumard from the Eagle-
ford near Woodlake, Grayson County; and S. vermicosus Shumard from
the Navarro near Dresden, Navarro County.
ENGONOCERAS SERPENTINUM (Cragin)
PI. 4, figs. 3, 5-6, 12
1900: Sphenodiscus belviderensis, var. serpentinus Cragin, Colo. Coll. Stud., viii, p. 31,
pi. 2, figs. 4-6.
1903: Engonoceras serpentinum Hyatt, U. S. G. S., Mon. XLIV, p. 162, pi. XIX,
figs. 7-14; pi. XX, figs. 1-5.
1918: Engonoceras serpentinum Stephenson, U. S. G. S., Prof. Paper 120-H, p. 143.
This distinctive Engonoceras is frequent in the shales of the Middle
Weno formation in Grayson and Cooke counties, Texas. Shell nacreous
in the material studied, with fine, close, sigmoid, radial striae; suture
simple, as figured by Hyatt (U. S. G. S., Mon. XLIV, pi. XIX, fig. 7) ;
venter rather square, angulated and rounded at edges, zigzag due to
alternating marginal tubercles on the two flanks.
HORIZON: Lower and Middle Weno shale and ironstone; Pawpaw
shale.
LOCALITIES : Frisco cut, three-fourths mile north of Union Station,
Denison, Texas, and the cut of Duck Creek just west of this locality; pit
of brickyard, one and three-fourths miles southeast of Gainesville, Texas ;
Pawpaw bluff on the Red River, northwest of Cedar Mills, Texas.
Weno and Pawpaw Formations 85
ENGONOCERAS sp.
PI. 4, figs. 8-10
The most numerous fossil in the basal Pawpaw clay is Engonoceras;
this genus is rare in the Duck Creek, Denton, Grayson, and Del Rio pyrite
faunae, and its abundance is diagnostic for the Pawpaw clay as so far
examined. There is probably more than one species in this formation.
The individuals are small (one inch or less), hematitic or pyritic, with
sharply etched sutures; flanks smooth and nearly flat; venter straight-
edged, angulated, concaved on the midline (so far as observed never acute
as in Metengonoceras) ; umbilicus narrow; sutures of varying complexity,
mainly very simple, with numerous auxiliary elements.
HORIZON: Pawpaw formation, clay facies, abundant: Tarrant
County, numerous localities; Denton County, Johnson County.
Grayson formation : marl facies and middle clay member, rare, Tarrant
and Denton counties.
Denton clay : rare, Denison to Blue Mound, north of Fort Worth.
Duck Creek marl: rare, Grayson to Tarrant counties.
FLICKIA BOESEI n. sp.
PI. 1, figs. 1-3
1920: Flickia sp. Winton and Adkins, Univ. Texas Bull. 1931, p. 69.
HORIZON : Pawpaw formation, clay facies, base.
LOCALITY : Type individual, base of Pawpaw formation, just or
top of Weno limestone escarpment, one-fourth mile east of Riovista-Waco
road and one mile south of Riovista, Texas. One eroded individual, the
type, was found here.
MEASUREMENTS : Height of last whorl, 3.5 mm., width, 4.6 mm. ;
greatest diameter, 10.5 mm ; width of umbilicus, 3.7 mm.
DESCRIPTION: Form discoidal, inflated, volutions thick, with thick,
crescentic section, moderately embracing, umbilicus deep, open, showing
at least five volutions. Cast smooth and unornamented.
From the section of the end of the coil it is evident that the volution
at this age embraces only about half of the preceding one; the volutions
are also much broader and lower than in the adult Flickia simplex, having
at the end of the fifth (?) volution a ratio of breadth to height of 3:2.
The flank is broadly convex and passes into the umbilical wall by a sharp
86 University of Texas Bulletin
convexity of more than a right angle. The curvature of the venter is
nearly elliptical ; a keel is lacking, but at the ventral midline of the latest
part of the coil there is a perceptible rounded angulation. The dorsal
region of the last volution has a more nearly circular curvature than the
venter, and the venter of the next younger volution is therefore taller
and more nearly circular than the outer volution.
SUTURE : Goniatitic, as in Flickia simplex Pervinquiere, from which
it differs only in minor details. All of the sutural elements are less tall
and relatively less slender than in the African species. As in that species
there are three lateral saddles and three lateral lobes; of these the first
and second lateral saddles and most of the second lateral lobe lie upon the
flank, while the remainder of the visible suture lies On the steep umbilical
wall. The siphonal lobe is bifid with two low, rounded points and a cen-
tral (external) saddle; the saddle has a greater breadth and is considerably
less pointed than the lobules, in fact it has a very broad, even, arcuate
curvature. The first lateral saddle is broad, non-angulate, evenly curved
and almost as tall as broad; its breadth occupies nearly half that of the
flank. The first lateral lobe and the second lateral saddle have almost
the same size and shape: each is rounded terminally, having almost a
circular curvature, and slightly more constricted basally; and the second
lateral saddle has in one instance a very slight suggestion of angularity,
like Neolobites. The second lateral lobe and the third lateral saddle are
low, broad and non-angular. The foregoing description is from the type
individual.
Fig. 9. Flickia boesei n. sp., type individual, sutures, camera lucida drawing, x 8.
Pervinquiere1 established the genus and species Flickia simplex to in-
clude a small ammonite with simplified suture remotely like Neolobites,
from the Vraconnian of Tunis. Comparing the latest sutures of the
two types,2 ' we find that the first lateral saddle of the Texas species is
somewhat lower and broader than that of Flickia simplex; the second
one is higher and lies entirely upon the flank, while in the African species
it appears to lie partly upon the umbilical wall; the external saddle of
Pervinquiere: Et. pal. tun., p. 212, pi. 9, figs. 2-5, text figs. 80, 82.
Weno and Pawpaw Formations 87
Flickia boesei is lower and more flattened than that of F. simplex; and
the siphonal lobe is narrower and taller and instead of being inflated,1
tapers slightly to the end. The Texas type is probably juvenile, since
the living chamber is lacking, and since it is more similar to the younger
than to the older sutures of Flickia simplex.
Such simplified ammonites afford few visible characters for comparison,
and therefore separations must be*made on the basis of slight superficial
differences. Very likely better preserved material will afford a more
secure basis for distinguishing the species and for defining its relation-
ships. Provisionally it is placed in Flickia on account of its form ana
suture. Since the species differs only slightly in form, cross-section and
suture from Flickia simplex, essentially the same arguments as to its gen-
eric position hold. It is notable, however, that in the Texas species the
resemblance to Neolobites suggested by Pefvinquiere is even more striking
than in Flickia simplex, especially in the very slight angularity of the
saddles.
FLICKIA (?) BOSQUENSIS n. sp.
PI. 1, fig. 4; PI. 4, fig. 11
There has recently come to light a peculiar Flickia-like ammonite, which
although not belonging to this genus as described by Pervinquiere seems
to stand closer to it than to any other genus, and is here described on
account of the possible light that it may throw on the relations of this
obscure group. This ammonite has prominent umbilical tubercles and a
few widely spaced low, rounded, coarse ribs, and the marginal tubercles
are lacking. In these respects it agrees with Neolobites, but is thicker,
more discoidal, has a more rounded keel, a more open umbilicus, and the
suture consists of three saddles and two lobes, the first saddle being much
taller and broader than the second. It will be seen that the suture has
fewer elements than in Neolobites, and in this respect is like Flickia. The
suture resembles that of Flickia in the simplicity, the roundness and the
non-angularity of its elements; it differs in having the siphonal lobe
broader and its sides more convergent towards the tip, the first lateral
lobe shorter than the siphonal lobe, and the first lateral saddle much
broader than the siphonal lobe. It differs from Flickia simplex and
F. boesei in having ribs and umbilical tubercles instead of being smooth.
The sutures on this ammonite are more numerous and crowded than in
either genus mentioned. Due to lack of literature, a more exact generic
determination can not be given.
1Ibid., Pervinquiere, p. 214, figx 82.
88 University of Texas Bulletin
HORIZON: Top of lower half of the Del Rio clay, equivalent of Gray-
son formation (top of zone of Exogyra arietina, in association with
Turrilites bosquensis, Acanthoceras worthense, Pecten subalpinus, Gryphea
mucronata) .
TYPE LOCALITY : West bank of the South Bosque River, 150 yards
south of the bridge on the Speeglevilte road, tall Del Rio cliff; 5.5 miles
west of courthouse at Waco, Texas.
DESCRIPTION : Form inflated, section of volution rather tall, flanks
and venter broadly rounded, keel absent, dorsum concave with a sharper
curvature than the venter ; volution covering about one-third of preceding
one. Volutions with few widely spaced, very large, smooth, low umbil-
ical tubercles each one-third to one-half the height of the volution; from
each of these a single low broad rib runs ventrally, reducing in height
and disappearing at the ventro-lateral margin. Ventral marginal tubercles
absent. Umbilicus wide. Only three volutions visible in the type (in-
terior damaged). The form is approximately that of Flickia boesei ex-
cept for the presence of ribs and the much more open umbilicus. In the
type the crowded sutures end abruptly near the end of the last volution,
beyond, which the living chamber has several oblique low ribs each term-
inating in a low, indistinct umbilical tubercle.
SUTURE: In form the suture is rather like that of Flickia or of
Neolobites, with a slight angularity in some places. Three lobes and three
saddles visible on each side, including the siphonal lobe. Siphonal lobe
Fig. 10. Flickia (?) bosquensis n. sp., diagrammatic projection of sutures of type
individual, camera lucida drawing, x 5.
subquadrate in outline, with two equal, simple, rounded lobules and a
shallow external saddle. First lateral saddle about one and two-thirds
times as broad as the siphonal lobe, more angular on its ventral margin,
more evenly curved dorsally. First lateral lobe about half as broad as
Weno and Pawpaw Formations 89
first saddle, lower than first saddle or siphonal lobe. Second saddle still
lower, about one and a half times as tall as the first lobe. Second lobe
nearly as broad as second saddle, and somewhat lower. Most of third
saddle visible externally, lying entirely on steep umbilical wall. Further
elements of suture concealed by overlap on next inner volution. All su-
tural elements are simple and entire, as in Flickia.
SCHLOENBACHIA WENOENSIS n. sp.
PI. 1, fig. 14
MEASUREMENTS: (Type individual).
Height of volution, 8.0 mm.
Width of volution, 4.7 mm.
HORIZON : Base of Pawpaw formation, clay phase.
LOCALITY : 723 (type locality) ; 714, both on Sycamore Creek, near
Fort Worth, Texas. The species is rather rare; only a few fragments,
most of them crushed, have been found.
The genus Schloenbachia Neumayr, in the restricted sense adopted by
de Grossouvre, Pervinquiere and others, includes ammonites with sinuous
simple or branched ribs, umbilical and marginal tubercles, and sutures
with the first lateral lobe usually trifid. Mortoniceras on the contrary
usually has a square cross-section, coarse, almost straight, tuberculate ribs
and the suture less dissected than in Schloenbachia, with the first lateral
lobe more or less square and bifid. The type species are Mortoniceras
texanum (Roemer) and Schloenbachia varians (Mantell). A rather rare
pyritic species of the Pawpaw clay is here described on account of its
stratigraphic importance.
DESCRIPTION: Form discoidal, volutions rather flat and broad
moderately embracing, outer volution covering about one-third the width
of the preceding one, umbilicus therefore wide and open and, on account
of the flatness of the volutions, rather shallow; three coils only exposed
in the type (fragment), the two inner ones being practically smooth, the
outer one decorated with numerous, closely spaced, low, evenly rounded,
sigmoidal, branched and simple ribs, most of them having distinct, sharply
elevated umbilical tubercles, which are nearly of even height and evenly
spaced around the inner margin of the volution ; and near the ventral
margin a low overturned, sharp-topped, oblique ridge representing the
twin marginal tubercles. On this ridge the more dorsally situated tubercle
is represented by a gently curved elevation and the more ventral tubercle
is sharper-topped and descends abruptly by a steep ridge and becomes
90 University of Texas Bulletin
obsolete at a point near the keel, leaving practically no groove bordering
the keel. The ribs, on this ridge, have sigmoidal flexures directed for-
wards, while at the umbilical margin the ribs are directed backwards.
The keel is sharp-topped, triangular in section, and elevated above the
level of the lateral tubercles. The section of the volution is rectangular
and slightly broader dorsally. At the widest point on the volution its
height and breadth are in the ratio of 3 :2. The section is thus truncate-
cuneiform; the flanks are practically straight, the venter lightly arcuate,
and the dorsum has a V-shaped excavation for the reception of the next
inner volution.
SCHLOENBACHIA WINTONI n. sp.
PI. 3, figs. 8-11
1920: Sehloenbachia sp. M, Adkins and Winton, Univ. Texas Bull. 1945, p. 34, pi. 5,
figs. 1-4.
1920: Sehloenbachia sp. M, Winton and Adkins, Univ. Texas Bull. 1931, p. 22.
MEASUREMENTS : ( Type individual ) .
Greatest height of last volution 34 mm.
Greatest breadth of last volution, excluding tubercles 32 mm.
Greatest diameter of shell . 104 mm.
HORIZON: Upper Weno formation, shale and limestone facies, and
ironstone bands in the blue shale of the Red River region. Known also
from south-central Texas.
LOCALITIES: 601, clay-ironstone layers in blue shale of upper part
of Weno formation, pit of brickyards, one and three-fourths miles south-
east of Gainesville, Texas (type locality) ; 604, cut of Frisco track, three-
fourth mile north of Union Station, Denison, Texas; 612, 618, 714, 715,
716, near Fort Worth, Texas ; 720, 721, near Riovista, Texas.
DESCRIPTION: Shell discoidal, volutions thickened, umbilical wall
steep, passing onto the flank by a rounded curve. Venter truncate, keel
low with a parallel groove on each side. Flanks slightly convex between
the ribs. Cross-section of volution subquadrate, slightly wider dorsally
than ventrally. Flanks ornamented with ribs, each connected with a ven-
tro-marginal tubercle. These ribs are either simple or bifid. The simple
ribs disappear dorsally before reaching the umbilical angle. The bifid
ribs end dorsally in a single, very tall umbilical tubercle and ventrally
in two less elevated marginal tubercles.
Visible portion of suture consists of siphonal lobe, two lateral saddles
Weno and Pawpaw Formations 91
and two lateral lobes. The siphonal lobe is about twice as tall as broad,
and laterally is minutely dissected, and has also two or three prominent
lateral inflections. The terminal points are slender and slightly incised
laterally. The first lateral saddle is nearly twice as broad as the siphonal
lobe and is trifid, having the more dorsal division slightly dissected, the
broader central division trifid, and the slender ventral division next to the
siphonal lobe entire. The deepest incision in the saddle lies between the
first two divisions. The first lateral lobe is slender and about two and
Fig. 11. Schloenbachia, wintoni n. sp., type individual, last suture, camera lucida draw-
ing, x 5. Keel region slightly distorted in type individual.
one-half times as tall as broad. It is bifid terminally and the ventral
lobule is larger. Each lobule is trifid. The selond saddle is lower and
broader than the first lobe, and is bifid terminally; laterally it has an ir-
regular outline. The second lobe is broad and bifid. The internal suture
has not been examined.
This species differs from Schloenbachia nodosa Bose and S. trinodosa
Bose in its suture and in the cross-section of the volution ; it differs from
the common Schloenbachia of the Fort Worth limestone (S. leonensis of
various authors) in many respects, notably in its marginal tubercles.
MORTONICERAS WORTHENSE n. sp.
PI. 1, figs. 6-10, 18-19, 26
1920: Mortoniceras sp. Winton and Adkins, Univ. Texas Bull. 1931, p. 68.
MEASUREMENTS: I (tpe) II III IV
Fragment, outer whorl ; length 15.0 16.5 14.4 10.8
Small end, height 3.5 4.3 3.0 2.4
92 University of Texas Bulletin
Small end, width 4.0 4.0 4.0 3.1
Large end, height 4.5 5.5 5.3 4.0
Large end, width 4.3 4.8 4.7 3.6
HORIZON: Basal two-thirds of the Pawpaw formation, clay phase.
LOCALITY : 723 (type locality) ; 714, and other localities near Fort
Worth, Texas.
DESCRIPTION: Shell discoidal, volutions slightly embracing, each
covering one-fourth or less of the next inner volution, umbilicus conse-
quently broad, volutions strongly ribbed with widely spaced, coarse, short,
simple or bifurcated, straight ribs, each with an umbilical tubercle and a
pair of coarse marginal tubercles which are connected by a concave topped
ridge. These tubercles are abruptly raised above the level of the venter,
but the oblique rapidly diminishing rib passes from the tubercle towards
the keel and becomes obsolete; the keel is therefore bounded on each side
by a narrow valley. Keel prominent, steep sided, triangular in section,
taller than the outer ventro-lateral tubercle in the earlier volutions, lower
in the later ones. Cross-section of the volutions roughly square, but in
a few individuals even broader1 than tall ; to be more detailed, the flanks
are inflated, and in the region of a rib bicarinate, corresponding to the
umbilical and lateral tubercles; venter tricarinate, corresponding to the
keel and the two ventro-lateral tubercles; dorsal midline with a slight
excavation, into which the next inner coil fits. Number of volutions six
or more. At the 6 mm: stage (about four volutions) the shell is prac-
tically without ribs. The ribs then come in as straight, broad, low, wedge-
shaped elevations, thicker and higher at the marginal end, where the
pair of marginal tubercles is an elongate prominence with a slight tuber-
culate swelling at each end. Within the next half volution the umbilical
tubercles have become prominent, and the marginal tubercles are as tall
as the keel, giving to the cross-section of the volution a nearly square
aspect, instead of the triangular section which exists in the younger stages,
in which the keel is still prominent. The sutures coincidently increase in
complexity.
SUTURE : The siphonal lobe is nearly quadrate. It is bifid and each
lobule is relatively simple. The first saddle is broad and is twice bifid.
The remainder of the suture is invisible on the flanks of the individuals
at hand, which are preserved as pseudomorphs of coarse grained hematite
which has replaced all structures and destroyed the details. From the
ends of fragments broken along suture lines it is inferred that the first
lateral lobe is lower than the first saddle and about two-thirds as broad;
terminally it is divided and possibly is trifid. The second saddle is lower
Weno and Pawpaw Formations 93
and narrower than the first lobe, and apparently is bifid; it lies at the
level of the dorso-marginai tubercles. The second lobe lies on the um-
bilical wall and is broad and flat, but from the material at hand its de-
tails can not be described. Between it and the tall narrow anti-siphonal
lobe there is a depressed saddle-like space. This description and figure
of sutures are taken from the individual figured on plate 1, figure 6.
Fig. 12. Mortoniceras worthense n. sp., suture of individual, Plate 1, Figure 6, camera
lucida drawing, x 10.
This species has similarities to Mortoniceras inflatum var. spinosum
Pervinquiere1 (Vraconian of Tunis). One individual of five volutions
has two gaps in the ribbing of the last volution; they have no obvious
relation to the branching or doubling of ribs. The same feature is noted
in the earlier volutions in this species.
ACANTHOCERAS WORTHENSE n. »P.
PI. 1, figs. 11-13, 16-17, 20-25
1920: Acanthoceras sp. Winton and Adkins, Univ. Texas Bull. 1931, p. 69.
MEASUREMENTS : PI. 1, fig. 12 PI. 1, fig. 13
Type (I) II
Greatest diameter 14.9 mm. 13.8
Height of last whorl 6.0 mm. 6.0
Width of last whorl 6.0 mm. 5.0
Width of umbilicus 1.4 mm.(?) 1.0
HORIZON: Pawpaw formation, basal two-thirds, clay facies.
LOCALITY: 723 (type locality), near Fort Worth, Texas; 714, 715,
716, 719, 724, near Fort Worth, Texas. The species is generally abundant
in favorably weathered exposures of the clay phase.
DESCRIPTION: Shell discoidal, compressed, four or more volutions
considerably embracing, umbilicus consequently small ; shell keelless, sec-
'Et. pal. tun., p. 229, pi. xi, fig. 3a-b.
94 University of Texas Bulletin
tion of volution roughly oval, venter smooth in young individuals and
very slightly convex. In older individuals, however, there is a median
broad, low, very rounded swelling, similar to a median tubercle. In young
individuals the ribs become obsolete just ventral to the ventral marginal
tubercle, but in older individuals the ribs are continuous across the venter.
Ventro-marginal tubercles acute, one on each rib, becoming obsolete in
the later volutions. Ribs long and short, mainly unbranched. Dorso-
lateral (umbilical) tubercles few and scattered. Cross-section of earlier
whorls subrectangular, flanks straight, venter lightly convex, dorsum very
concave; in later whorls the flanks are more rounded and make an even
curve with the venter. In certain young individuals the ribs are flexuous,
having a prominent sigmoidal curve, and are much thickened at the mar-
ginal tubercle. This individual shows no ribs at a diameter less than
3.8 mm. After that diameter, the intercalated ribs, one or two between
some branches, are similar to those of the later volutions.
The suture of the species resembles that of young individuals of
A. martimpreyi Coquand, as figured by Pervinquiere.1 The considerable
Fig. 13. Acanthoceras worthense n. sp., suture, camera lucida drawing, x 8.
amount of material at hand does not contain any sutures which are much
more complicated than the ones figured here. The suture shows exter-
nally besides the siphonal lobe, four saddles and four lobes, which pro-
gressively decrease in size toward the anti-siphonal region. The bifid
first saddle is more irregular and less square than in the examples of
A. martimpreyi mentioned. All the remaining saddles are simple, or
bifid, and the lobes are generally bifid. The first lobe is as tall as the first
iPervinquiere, Et. pal. tun., p. 294, figs. 109-110.
Weno and Pawpaw Formations 95
saddle and about three-fourths as broad. The second and third saddles
are taller than broad and rather angular in form. The remaining lobes
likewise are subquadrate and shallowly bifid. The internal suture has not
been examined.
This species greatly resembles Acanthoceras martimpreyi Coquand
A. aumalense Coquand, and A. suzannae Pervinquiere, all from the Vra-
conian of Tunis.
ASTEROIDEA
The genera of Comanchean starfishes are in such great need of defini-
tion that it has been found impossible to assign the Texas species with
much certainty to the proper genera ; for in the absence of authentic ma-
terial of described species it is difficult to make such definitions fron<
figures and text alone. When the Texas starfishes are closely defined it
will probably be necessary to form new genera for certain of the species,
but in the meantime they have been provisionally assigned to known
genera, avoiding when possible those founded on recent species, on ac-
count of the great amount of subdivision which the recent Asteroideo
are receiving at the hands of modern workers.
PENTAGONASTER TEXENSIS Adkins and Winton
PI. 7, fig. 7
1920 : Pentagonaster texensis Adkins and Winton, Univ. Texas Bull. 1945, p. 47, pi. 10,
figs. 5-6.
1920: Pentagonaster texensis Winton and Adkins, Univ. Texas Bull. 1931, p. 22.
A recently discovered individual shows the superomarginal plates, and
the interior of the disk is eroded down to the oral surface, of which several
adambulacral, circumoral, and a few paramarginal plates are exposed.
All of the superomarginal plates are shown, but due to erosion and the
thinness of the disk, certain oral plates come into view, and there is over
the disk a resulting mixture of oral and aboral plates. This individual
was found in a limestone slab, face down, at the type locality described
below.
HORIZON : Upper five feet of the Weno limestone.
LOCALITY: 602, east slope of the valley of Sycamore Creek, four
miles southeast of Fort Worth, Texas, at a level 29 feet below the base
of the Mainstreet limestone.
96 University of Texas Bulletin
DESCRIPTION:
SUPERO-MARGINAL PLATES: On each aboral interarc there are
fourteen supero-marginal plates excluding the terminal plate, which is
common to each two adjacent arcs. These plates, though separated, seem
well preserved, and in this individual as in the type, lack ornamentation.
It is entirely possible that better material will show superficial structure
on the plates since most related species show it. In shape the plates are
trapezoidal or cuneiform, as described for the type. They are tallest
and widest at the center of the arc and decrease in size to the tips of the
rays. The marginal plates of this species are relatively large and are
taller than broad ; in Pentagonaster browni Weller, they are broader than
tall, and are relatively smaller.
PARAMARGINAL PLATES : These are a row of minute, nearly equal
and similar subquadrate plates lying apposed to the inner edge of the
marginal plates. Only a few, near the tips of the rays, are preserved in
this individual; they apparently belong to the aboral surface.
ADAMBULACRAL PLATES : These plates, as described in the type,
are mostly quadrate and are of about the same size as the other interior
oral and aboral plates (about .5 mm. diameter). This individual has
along one radius two nearly apposed rows of plates that belong to this
class; they diminish in size somewhat toward the tip of the ray.
CIRCUMORAL PLATES: There is a group of plates massed around
the mouth region, which are in part oral plates and in part dislocated
central aboral plates. They are rounded and larger than the other interior
plates, and a few are elongate. In the absence of better material, they can
not be described more accurately.
INTERMEDIATE PLATES : There are a few continuous radial rows
of plates lying on the radii and extending from the center of the disk to
the tips of the rays. These are apparently aboral plates. They have a
rounded, roughly quadrate to hexagonal shape, and are small, equal and
similar. The madreporite and ambulacrai details are not visible.
RELATED SPECIES : Pentagonaster browni Weller (Fox Hills form-
ation, Lander, Wyoming) is described as having 16 supero-marginal plates
which are relatively smaller and less tall than in this species. The inter-
radial arcs of the Wyoming species are also deeper than in our material.
P. lunulatus Woodward and P. megaloplax Sladen (Upper Chalk, Senonian)
differ from the Texas species in having punctate or papillose marginal
plates, in the concavity of the interarcs, and in the number of marginal
plates. P. robustus Spencer (Upper Chalk) differs in the same charac-
ters and in the meeting of the supero-marginal plates along the midline
Weno and Pawpaw Formations 97
of the ray; and P. obtusus Forbes (Upper Chalk) is stated to have 18
marginal plates, the superior ones punctate and the two sets alternating.
I (type) II
R (average of five) 23.5 mm. 15.9 mm.
r (average of five) 14.8 mm. 9.9 mm.
R/r 1.58 1.6
METOPASTER HORTENSAE Adkins and Winton
PI. 7, fig. 6
1920: Metopaster hortensae Adkins and Winton, Univ. Texas Bull. 1845, p. 46, pi. 10.
figs. 2-4.
1920: Metopaster sp. Winton and Adkins, Univ. Texas Bull. 1931, p. 69.
1920: Metopaster hortensae Winton and Adkins, ibid., p. 21.
This rare species, which characterizes the basal Pawpaw clay, has very
tuberculated and spiny plates. The marginals are covered with closely
set, low, rounded tubercles, and at places have adherent clumps of small
thick spines.
One row of ambulacral pore plates is shown on the type individual.
This has two rows of oblique pores, indicating four rows of tube-feet per
groove.
As already stated, there are six paired supero- and infero-marginals in
addition to the terminal unpaired supero-marginal plate, totalling eight
supero-marginals and six infero-marginals.
The terminal marginal plate is similar to that of Mitraster, which differs
from the Texas form in its cycloid contour and in the shape and ornamen-
tation of its marginal plates.
COMPTONIA WINTONI n. tp
PI. 7, figs. 4-5
1920: Comptonia sp. Adkins and Winton, Univ. Texas Bull. 1945, p. 49, pi. 10, fig. 1.
MEASUREMENTS:
Major radius, about 24 mm.
Minor radius (average) 6 mm.
DESCRIPTION: Disk flat although somewhat collapsed in the type.
Rays elongate, tapering, incomplete in the type; probably the ratio R:r is
about 4:1. Minor radius about 6 mm. in the type. Supero-marginal and
infero-marginal plates numerous, usually paired, disk relatively small and
98 University of Texas Bulletin
the interradial arcs next to the disk paraboloid, sharply instead of broadly
curved, and in this respect more similar to Comptonia comptoni Forbes
than to C. elegans Gray. The two rows of supero-marginal plates are
apparently nowhere in contact throughout the length of the ray. Oral
and aboral sides of disk covered with rather small, unequal, polygonal to
rounded raised plates.
ABORAL SIDE : The supero-marginal plates at the center of the arc
are slightly wedge-shaped with rounded interior margins ; their sides con-
verge slightly, passing out from the center of the disk. The plates de-
crease in size and are more elongate, on approaching the tip of the ray.
Over the central part of the arc seven plates have the breadth of about
10 mm. There are probably about 20 supero-marginal plates in one entire
arc (the tips of the rays are absent in the type) .
Along the center of each ray is a row of radial plates which are larger
than the other central plates but not elevated above them. One elevated
rounded plate on each interray bears a small circular pore (gonopore).
In one interray there are two such plates. Between these plates are more
depressed rows of plates arranged so as to make a pentagon with its cor-
ners at the interradii. The central radial rows of plates along the rays
meet the middles of the sides of this pentagon. The small, raised, oval
madreporite is situated excentrically, and bears 9 or 10 radiating mostly
divaricate, V-shaped straight ridges.
ORAL SIDE : The infero-marginal plates are equal in width and in num-
ber to the supero-marginal and lie opposite them or nearly so. The oral
surface of this starfish is distinctly broader than the aboral surface, so
that the line of junction of the two sets of marginals is situated well aboral
to the edge of the disk (and this does not seem to be due to crushing).
The infero-marginal plates are subquadrate-cuneiform in profile, but are
very thick and rounded at the external edge. No para-marerinal rows of
plates are visible. The other plates of the oral face of the disk, which
are poorly preserved, are also not in rows. The five ambulacral grooves
are distinct but without perceptible structure in our material. The num-
ber of rows of tube feet is unknown. The grooves are prominent, and
have near the peristome a breadth of about .6 mm. The marginal and
other larger plates are covered by rather fine, low, round, irregularly
scattered tubercles. Evidences of spine pits and pedicellariae are absent.
The species differs from Comptonia elegans Gray in several noticeable
features. The disk is practically flat in our species; it however, shows
some evidence of flattening in preservation, since the central plates are
considerably and abruptly depressed below the level of the supero-marginal
Weno and Pawpaw Formations 99
plates. Comptonia elegans on the other hand has a central ridge of very
rounded elevated plates running the length of each ray and connecting
to form on the disk a central, narrow, elevated ring. In our species the
center of the disk is flat and the plates are very little disarranged, since
the depression mentioned above has not disturbed the relations of the
central plates to each other.
Calliderma and Nymphaster differ from our species in many notable
features. Both have the aboral interadial areas in most species confined
to the disk, so that the supero-and infero-marginal plates meet over most
of the length of the ray. This is not true in the Texas species. Both
genera named were described from recent species, the genotypes being
Nymphaster protentus Sladen1 and Calliderma emma Gray.2
This species differs from Comptonia elegans Gray in several important
respects. The disk is practically flat in our species; it, however, shows
some evidence of flattening in preservation, since the central plates are
considerably and abruptly depressed below the level of the supero-marginal
plates. Comptonia elegans, on the other hand, has a central ridge of very
rounded elevated plates running the length of each ray and connecting
to form on the disk a central narrow elevated ring. In our species the
center of the disk is flat and the plates are very little disarranged, as the
foregoing description shows.
PENTACEROS AMERICANUS n. sp.
PI. 7, figs. 1-3
MEASUREMENTS: R (average of two) 45.0 mm.
r (average of five) 10.4 mm.
R:r 4.33:1
A species having the form of Pentaceros jurassicus Quenstedt and in
most respects agreeing with the described generic characters, is here re-
ferred to this genus.
HORIZON: Base of the Pawpaw formation, clay fades,
TYPE LOCALITY: 714, one-fourth mile south of the International
and Great Northern Railway bridge across Sycamore Creek, four and
one-half miles southeast of Fort Worth, Texas. One individual, the type,
was found here.
Sladen: Narrative of Challenger Exp., 1886, vol. 1, p. 612; Zool. Chal. Exp., part li,
Report on the Asteroidea, 1889, p. 294.
Fisher, W. K., Starfishes of the Philippine seas and adjacent waters. U. S. N. M.
Bull. 100, vol. 3, p. 261, 1919.
2Gray: Proc. Zool. Soc. Lond., part XV, 1847, p. 76; Ann. Mag. Nat. Hist., 1847
vol. XX, p. 198; Synopsis of Species of Starfish, British Museum, 1886, p. 7.
100 University of Texas Bulletin
TYPE INDIVIDUAL : A well preserved individual showing both sides
of the disk in great detail and having two complete and three fragmentary
rays. Museum of Texas Christian University, Fort Worth, Texas.
DECRIPTION : Marginal plates distinct, subrectangular on edge
view, rounded on the face, bearing fine tubercles. Inter-marginalia pres-
ent in the interarcs and the proximal half of the rays, decreasing in size
outwards from the disk. Disk relatively small, arcs sharply rounded, rays
long and slender; oral surface flat with numerous small plates; aboral
surface with a central raised pentagonal system of plates and a row of
radiating plates on the midline of each ray.
ABORAL SIDE : The rays are slender and the interarcs sharply
curved. Each interarc contains from tip to tip of the rays 48 supero-
marginal plates (17+7 in each half arc) . Of these all except the terminal
seven of each ray are elongate in the direction of the ray, sharply rounded
on top and separated from those of the opposite side of the ray by radial
plates. The terminal seven plates of each margin of the ray are apposed
along the mid-line; the plates are transversely elongate and join by alter-
nate facetting, along a zigzag line; the terminal plate is unpaired and
is common to the two rows. The seven terminal plates are swollen and
smooth and present a very different appearance from the others. In the
type they are smooth and whitish, lacking the iron stain of the rest of
the animal. A single row of radials extends from the inner pair of these
terminal plates to a polygonal elevation in the center of the disk, the plates
increasing in size towards the disk. Between this row of plates and the
supero-marginal plates there are two parallel rows of plates, an adradial
row of large plates fitting into the spaces between the radialia, and a
para-marginal row of small cuboidal plates lying against the marginal
plates, there being about three of these plates to one marginal plate.
The interradial areas on the disk are triangular and are covered with
three or four rows of small plates lying close to the marginals; at the
apex of each area is a perforated, elevated polygonal plate, the genital
plate with its gonopore. The radial ridges running on the mid-line of
the ray near the disk are composed of three irregular rows of large rounded
ossicles and numerous smaller scattered plates, which were apparently
imbedded in a membrane. The central polygonal ring-like elevation at
their union bears scattered large and small ossicles. The anus is sub-
central and large ; the madreporite is excentric, raised, hexagonal in shape,
depressed in the center, and has coarse imbricated V-shaped ridges, and
straight, simple or branching ridges, radiating from the center.
ORAL SIDE : The oral side is strikingly flattened, being only slightly
compressed along the ambulacral grooves. Its prevailingly smooth ap-
Weno and Pawpaw Formations
pearance is due to the smallness and flatness of the numerous ptales: #hi(5h
make up its area. Infero-marginal plates as described for the supero-
marginals, and paired with them; however, there are only six inflated
terminal plates separated to the tip of the ray by the ambulacral groove:
The common terminal closing plate is restricted to the aboral side. Infero-
marginal plates finely granulose.
Interambulacral areas of oral side broadly triangular with numerous
crescentic, coarsely granulated small plates in roughly concentric rows.
An adambulacral row of plates with combs of spines lies next to the
ambulacral grooves. Between these and the marginals is one row of
plates over most of the length of the ray, but on approaching the inter-
radial areas other rows enter. Peristome central, apparently protected
by fine incurved spines.
The species resembles in form Nymphaster radiatus Spencer (Lower
Chalk, Upper Cenomanian), from which it differs in the shape and orna-
mentation of its marginal plates. It also has resemblances to Pentaceros
boysii Forbes and P. squamatus Forbes, both from the Upper Chalk of
Kent, England (Senonian), but it differs in these in its form and in the
ornamentation of the plates.
ECHINOIDEA
LEIOCIDARIS SP.
Cidarids are known from all the Texas Washita formations above the
Fort Worth limestone. These are undescribed and their tests and spines
unrelated with one exception, Leiocidaris hemigranosus Shumard from
the Denton formation, of which spines and test have been found in such
close proximity that they almost certainly belong to the same animal.
Cidarid plates, apparently of a Leiocidaris, are abundant in the Quarry
limestone group of the Red River region and with them occur great num-
bers of spines. In addition, in the Pawpaw clay and in the Grayson marls
there are several different species of large cidarid spines. In the Main-
street limestone well preserved cidarid tests are known.
Cidarid sp. 1, spine: The commonest echinoid spine of the Quarry group has the
following characteristics :
The shaft bears about sixteen carinae which are made up of rows of rounded, bead-
like tubercles, whose tips are slightly pointed down the shaft. The rows are even
topped and depressed. On some spines certain carinae are elevated considerably above
others and are longer, more prominent, and have a sharp serrate keel and a triangular
cross-section. The spine is a short oval in cross-section. Below the tip of the shaft
several, in part alternate, carinae end, and the remaining ones become more elevated
102 University of Texas Bulletin
p.nd- sharp keeled, .giving to the shaft a Cereus-like appearance. At the base of the
spine there is an inflated sharp topped milled collar; the condyle is constricted and the
articulating surface deeply excavated. Locality: 601, near Gainesville, Texas; widely
distributed in North Texas.
Cidarid sp. 2, spine: Cidarid spines of medium length, the shaft not inflated. The
shaft bears about 30 depressed, even topped, equal and equally spaced continuous lines.
The base is gently inflated and straight sided down to the collar. The collar is not
milled and is rounded, making a wide angle with the shaft. The straight margin of
the base below the collar descends to the rim of the circular articulating socket. This
spine differs from the preceding in having numerous nonserrate carinae. Locality:
601, pit of brickyards, near Gainesville, Texas.
Cidarid sp. 3, spine: Spines with an inflated, club-like shaft bearing about 10
• sharply but unequally elevated, smooth keeled carinae and a prominently constricted
neck. The margins of the base above and below the collar are smooth and straight
and make at the collar a rounded angle of about 135 degrees. The rim of the cir-
cular articulating socket is a ring-like thickening. Cross section of inflated shaft ang-
uJar and subcircular. Locality: 601, pit of brickyards near Gainesville, Texas, Quarrj
limestone.
GONIOPYGUS .p.
A species of Gonipygus from the basal five feet of the Pawpaw forma-
tion clay facies, locality 714, near Fort Worth, Texas, is in the hands of
Professor F. L. Whitney for description.
PEDINOPSIS SYMMETRICA (Cragin)
1893: Dumblea symmetrica Cragin, Geol. Surv. Texas, 4th Ann., Kept., p. 150, pi. xxiv,1
fig. 12; pi. xxv, figs. 4-7; pi. xxvii, fig. 1.
1915: Pedinopsis symmetrica Clark, U. S. G. S., Mon. LIV, p. 64, pi. xxiii, figs. 1 a-h
Three individuals of this species found in the basal Weno marl, locality
618, near Fort Worth, Texas, have been placed in the hands of Professor
F. L. Whitney for description.
PELTASTES sp.
A poorly preserved individual somewhat similar to a Peltastes found
in the topmost stratum of the Mainstreet limestone at Denison, Texas,
was found at locality 714, near Fort Worth, Texas, in the basal stratum
of the Pawpaw clay, and it is referred to this genus. These echinoids
will be described by Professor F. L. Whitney.
Erroneously cited as pi. xxxiv by Cragin and Clark.
Weno and Pawpaw Formations 103
SALENIA sp.
A large flattened Salenia, resembling in form S. mexicana Schltiter,
which is not known to range so high, was found in the basal stratum of
the Weno formation, just on top of the Gryphea washitaensis shell con-
glomerate of the Denton marl, by the St. Louis and San Francisco Railway
track, two and one-half miles north of Denison, Texas.
The following are some of the features of this individual: There are
about 20 pairs of ambulacral tubercles, obliquely situated ; the ambulacral
lips are considerably wider than the inter-ambulacral lips ; the apical sys-
tem ("cap") is large, the plates ornately scalloped; the sutures are widely
and irregularly excavated. . ^
Salenidae have so far been found at the following levels in the Texas
Comanchean :
Buda: S. volana.
Grayson: Peltastes sp.: Goniophorus sp.
Mainstreet: .
Pawpaw: Peltastes? sp., Salenia volana.
Weno: Salenia sp. aff. texana.
Denton: Goniophorus sp.
Duck Creek marl: Goniophorus sp.
Duck Creek limestone: Salenia sp.
Goodland limestone: Salenia mexicana, S. texana, Salenia n. sp.
Walnut: S. mexicana; S. n. sp.
Glenrose: Salenia n. sp.
CYPHOSOMA VOLANUM Cragin
This widespread Upper Washita species is occasional in the Weno form-
ation, marl facies, in association with a considerable echinoid fauna and
other fossils, such as Turritella worthensis, Venericardia worthensis,
Remondia ? acuminata and Ancycloceras bendirei. It is known otherwise
from the Weno to the Buda limestone.
HOLECTYPUS LIMITIS Bose
This species is distinguished from Holectypus planatus Roemer by hav-
ing the periproct in length about half the radius of the test and situated
about halfway between the centrally located peristome and the ambitus,
while the Holectypus planatus the periproct occupies almost the entire
length between the peristome and the ambitus. This species, described
from subdivision 5 of Cerro de Muleros (Duck Creek and Fort Worth
formations) occurs in the Upper Washita beds of North Texas as
104 University of Texas Bulletin
Holectypus planatus does in the Lower Washita and Fredericksburg beds.
It is scattering in the Weno and Pawpaw formations but more abundant
in the echinoid horizon at the base of the marl phase of the Weno forma-
tion, in association with Enallaster bravoensis, E. wenoensis, Hemiaster
riovistae, Epiaster wenoensis, Pedinopsis symmetrica and Holaster. It is
sparse in the Mainstreet formation and has a zone of abundance near the
base of the Grayson marl.
HOLASTER sp. aff. SIMPLEX Shumard
HORIZON: Weno formation, marl facies, abundant near base; Paw-
paw formation, marl facies, occasional near top.
LOCALITIES: 611, 612, 618, 715, 716, 718, near Fort Worth, Texas;
721, 722, near Riovista, Texas; cut of Missouri, Kansas and Texas Railway,
one mile north of Union Station, Denison, Texas, between localities 605
and 606.
The common Holasters of the Weno and Pawpaw formations have close
similarities with the low phase of Holaster simplex Shumard of the Duck
Creek and Fort Worth formations, but are specifically distinct. How-
ever, it is considered best to defer their description awaiting better ma-
terial. These echinoids occur as eroded mud-filled, calcite tests and the
ambulacral areas and apical system are almost invariably damaged.
Tests ovoid in outline, non-angular, anterior notch shallow, longer than
tall, greatest perimeter generally above the base.
Ambulacra flush with surface, postero-laterals in some individuals more
divergent than in H. simplex; peristome transverse, oval, lying in a de-
pressed space near the ambitus. Peripcroct low, ovoid, vertically elongate
lying in tall individuals beneath a prominent posterior median projection.
Apical system subcentral elongate.
It should be borne in mind that the Holasters of the Weno marl are
diverse, and that among them Holaster simplex may occur, since its known
stratigraphic range extends into the upper Fort Worth limestone.
The species of Holaster closely related to H. simplex Shumard of the
Duck Creek and Fort Worth formations, and found in the Weno and Paw-
paw formations shows the same variation in form as the lower species;
sloping individuals with their greater perimeter at the base, and top-heavy
individuals with the greatest perimeter above the base, are common, the
latter being most abundant. This species seems to differ from H. simplex
in the shape of the madreporite which is elongate instead of subquadrate
and in details of the apical system. Since such species are not easily de-
finable by form alone, it has been thought advisable not to describe the
Weno and Pawpaw Formations 105
Weno species until more material is available. Cragin1 described three
species of Holaster, some of which are valid species. Holaster supemus
Cragin (Grayson marl, Argyle, Texas), a top-heavy echinoid with a cir-
cular apical system, is a Stenonia. The small low species, H. nanus, from
the "Vola bed" (Mainstreet?) on the Denison-Bonham road, Choctaw
Creek, Grayson County, Texas, is apparently the same low species that is
common in the Weno and Pawpaw formations throughout North Texas.
The other species, H. completus, which was found in the "Denison beds"
and the Mainstreet limestone in Goyson County, has a very distinctive
apical system, but has the periproct infra-marginal, and is not a Holaster.
In addition, a very small pyritic Holaster whose characters are too im-
perfectly known to warrant description, occurs in the basal Pawpaw clay.
EPIASTER WENOENSIS n. sp.
PI. 6, fig. 6
MEASUREMENTS:
Type: Length 54 mm.
Breadth 50 mm.
Height 29 mm.
Apical system to posterior border 32.5 mm.
HORIZON : Weno and Pawpaw formations, most abundant in the basal
third of the Weno, marl facies, in association with Holaster sp. aff. simplex
Shumard, Enallaster bravoensis Bose, E. wenoensis n. sp., Hemiaster cal-
vini Clark and H. sp. aff. bexari Clark.
LOCALITIES: 618, near International and Great Northern Railway
track, three miles southeast of Fort Worth, Texas (type locality). 602,
611, 612, near Fort Worth, Texas ; near Riovista and Blum, Texas ; three
miles north of Gainesville, Texas; Missouri, Kansas and Texas Railway
cut one mile north of Union Station, Denison, Texas; and elsewhere gen-
erally distributed in the North Texas Weno. Localities 714, 715, 718, 723,
and other Pawpaw localities near Fort Worth, Texas, especially in the
upper marly portion of the Pawpaw.
DESCRIPTION : Superficially similar to Hemiaster elegans Shumard,
but smaller, smoother, less inflated, less bulged between the ambulacral
grooves, and with straighter and narrower ambulacra. The species re-
sembles E. aguilerae Bose, but is smaller and differs in the form and am-
bulacral details. The Texas Comanchean Epiasters may be distinguished
'Cragin, Geol. Surv. Texas, 4th Ann. Kept, pp. 165-168. '
106 University of Texas Bulletin
from Hemiaster calvini and others by the absence of a conspicuous tubercle
between the pores of a pair in the unpaired ambulacrum and usually by
the larger size, the slighter depression of the ambulacral grooves, and the
shape of the test. It is stated that Hemiaster has peripetalous fascicles
while Epiaster lacks them ; but this character is of no value in the usual
Texas material, which entirely lacks fascicles. Hemiaster elegans and
Epiaster aguilerae are of large size, while Hemiaster whitei and Epiaster
wenoensis are of medium and small size.
Test: Inflated, rotund, smooth, ambulacra nearly straight, only slightly
depressed. Widest point of test just anterior of apical system, tallest
point on mid-line posterior to apical system and one-third the distance
from it to the ambitus. Sides inflated, rather straight, greatest peri-
meter at bottom. Aboral side nearly flat, peristome region excavated,
with a projecting keel on the posterior lip and the grooves of the antero-
laterals and the anterior sulcus slanting into the peristome. Posteriorly
on the oral mid-line the test is inflated, the most prominent point being
near the posterior end of the test. Ambitus rounded, with only an antero-
lateral angulation just back of the point where the antero-lateral ambul-
acra cross the ambitus; posteriorly the test has a rounded outline. Test
narrowed to a pointed, very narrowly truncate posterior end.
Unpaired ambulacrum lies in the shallow anterior sulcus, which is sim-
ilar in form to the other ambulacral grooves, but slightly narrower. Each
one has about thirty-one pairs of short slit-like pores set at a slight angle
to each other.
Antero-lateral ambulacra diverge at an angle of about 150 degrees,
then turn forwards slightly, being thereafter almost straight to the am-
bitus. Pore zones similar, with the pores almost equal. Each zone has
about fifty pore pairs, the pores being short, slit-like, and not set at an
angle to each other. Both pores of the anterior zone and the anterior
pores of the posterior zone are equal ; the posterior pores of the posterior
zone are about one and one-third times as long.
Postero-lateral ambulacra long, straight, diverge at an angle of about
60 degrees. About fifty-four pore pairs in each zone, pores slit-like, sim-
ilar and nearly equal, the interior ones being, however, shorter than the
exterior ones.
Peristomal ambulacral pores. The ambulacra after crossing the am-
bitus continue as smooth finely granulated strips of large plates with
reduced pores, and end at the peristome. However, on approaching the
peristome the pores become conspicuous and are borne on elevated knobs
with a crater-like opening to one side of the top. These are present in
the following Texas species examined : Epiaster wenoensis n. sp. (most
Weno and Pawpaw Formations 107
prominent), E. aguilerae Bose, Hemiaster elegans Shumard, H. whitei
Clark, H. sp. ( Fredericksburg division), H. calvini Clark. The antero-
lateral rows are conspicuous, consist of eight to nine cup-like elevations
decreasing in size outwards from the peristome, the cavities opening out-
wards and forwards in the anterior row, outwards and backwards in the
posterior row. Each cavity bears two nearly circular ambulacral pores,
placed obliquely. The antero-lateral and postero-lateral craters make two
V-shaped rows at their junctions back of the peristome. The postero-
lateral rows each contain about five similar, smaller craters which are
lower and more widely spaced farther from the peristome.
Peristome oval, the long axis transverse, the anterior curvature being
even, the posterior margin with a central, bluntly rounded, elevated, for-
wardly projecting lip.
Periproct rather similar to that of Epiaster aguilerae Bose: shape
trapezoid with the bottom and top rounded, the two superior angles being
sharply rounded and the superior margin but slightly arched; the sides
diverge, making the periproct broader at the bottom than at the top;
the inferior angles are broadly rounded and the inferior margin likewise,
it being nearly the arc of a circle of the same diameter as the periproct.
RELATED SPECIES: Epiaster wenoensis n. sp. is smaller than
E. aguilerae Bose; is more narrowed and pointed posteriorly; is less ele-
vated medially just posterior to the apical system, but farther posteriorly
is more straight-topped, the slope to the periproct being relatively abrupt ;
the notch made in the ambitus by the anterior sulcus is shallower and less
pronounced than in E. aguilerae; the peristomal ambulacral pores are
larger and more pronounced, more numerous and more crowded than in
any other Texas species examined ; the species is more smooth in appear-
ance and more sparsely tuberculated aborally than E. aguilerae Bose or
H. elegans Shumard.
The relations existing between Hemiaster, Epiaster and Macraster in
the Texas Comanchean have not been satisfactorily solved. Hill1 and
Clark- have considered Macraster texanus Roemer3 to be synonymous with
Hemiaster elegans Shumard.4 Roemer and Bose5 state that this species
comes from the Fredericksburg division, but Hill6 says that| it "makes a
well defined horizon near the very top of the immense thickness of lower
iHill, Annotated Check List, etc., Geol. Surv. Texas Bull. 4, p. 2, 1889.
'Clark and Twitchell, U. S. G. S. Mon. LIV, p. 88, 1916.
"Roemer, Neues Jahrb. f. Min., Geol. p. Pal., Bd. I, pp. 191-195. Tf. VI, 1888.
'Shumard, Pal. Exp. Red River of La. in 1852, p. 210, pi. II, fig. 4a-c, 1853.
5B6se, Inst. Geol. Mex. Bol. 25, p. 173, 1910.
"Hill, On the Occurrence of Macraster texanus, Amer. Nat., XXIII, p. 68, 1889.
108 University of Texas Bulletin
marine Cretaceous in Texas" (Buda limestone?) and is "not as Dr.
Roemer infers from the specimens which accompanied it to Germany:
with the Exogyra texana fauna, a statement which has been verified by
Mr. George Stolley, the collector."
The distinction between Hemiaster and Epiaster revolves around the
presence or absence of fascicles, and Clark' refers Epiaster elegans Auctt.
to the genus Hemiaster "as better material has shown that peripetalous
fascicles are present although poorly developed and commonly destroyed
on most specimens." There seems no a priori reason for doubting this
statement until well preserved material demonstrates the contrary.
Epiaster aguilerae Bose,2 a distinctive species of the lower Fort Worth
limestone, described from subdivision 5 of Cerro de Muleros near El Paso,
is here redescribed by comparison with E. wenoensis n. sp., an analagous
a'nd equally distinct species from the Upper Washita beds of North Texas.
In the collections of the Department of Geology, University of Texas, is an
unlabeled echinoid, probably an Epiaster wenoensis, and marked with
a red T, as many of Cragin's types were marked, but whether this is a
type, and of what, is unknown. Its dimensions, length 36.5 mm., breadth
34.0 mm., height 17.0 mm., do not agree with those of any Epiaster men-
tioned by Cragin, who described Epiaster electus (Travis Peak forma-
tion), E. elegans var. praenuntius (Comanche Peak limestone), E. hem-
iasterinus (Grayson formation), and E. whitei Clark (Travis Peak,
Comanche Peak and Fort Worth formations). Since Cragin's species are
unfigured and the types apparently lost, they are considered invalid species.
The present species differs from Hemiaster whitei Clark in being much
less tuberculate, in having narrow straight ambulacra in shallow grooves
instead of wide ambulacra in deep grooves ; the form is much wider, more
broadly rounded posteriorly, and distinctly lower; the slope anterior to
the apical system is steeper. In appearance this species can not be con-
fused with the common H. whitei Clark of the North Texas Goodland lime-
stone. Epiaster hemiasterinus Cragin is considered by Clark3 as identical
with Hemiaster whitei, and Cragin admits4 the "probable identity" of the
two. It is described as being tall, with deep ambulacral grooves.
iClark and Twitchell, U. S. G. S. Mon. LIV, p. 88, 1916.
2B6se, Inst. Geol. Hex., Bol. 25, .p. 173, pi. 47, figs. 2-4, 67; pi. 48, figs. 1, 2, 4, 1910
3Clark, U. S. G. S., Mon. LIV, p. 89, 1915.
4Cragin, Geol. Surv. Texas, 4th Ann. Kept., p. 155, 1893.
Weno and Pawpaw Formations 109
EPIASTER AGUILERAE Bose
PI. 5, fig. 5; PI. 8, fig. 7
1910: Epiaster aguilerae Bose, Inst. Geol. Mex., Bol. 25, p. 173, pi. 47, figs 2-4, 6-7;
pi. 48, figs. 1, 2, 4.
1920: Epiaster aguilerae Winton and Adkins, Univ. Texas Bull. 1931, p. 68.
MEASUREMENTS : Bose's
type I II
mm. mm. mm.
Length _ 77.2 66.2 48.0
Width 69.1 65.5 43.5
Height . 39.0 32.0 24.0
Apical system to posterior margin 43.9 37.0 29.0
Two individuals from the basal Fort Worth limestone near Fort Worth
are referred to this species, which was described from Subdivision 5 (Fort
Worth formation) of Cerro de Muleros on the basis of one imperfectly
preserved individual. The individual figured in this paper is of the same
proportions as Bose's individual but about one-seventh smaller. It differs
also in having the antero-lateral ambulacra diverge at a greater angle,
and in being slightly taller and longer from the apical system back : but
the last two features mentioned are due in part to a small amount of end-
wise crushing suffered by this fossil. In other respects it agrees with
Bose's description. This echinoid is proportionately broader and shorter
than the typical Fort Worth limestone, Hemiaster elegans Shumard, of the
form figured by Adkins and Winton1 and has a decidedly rounded, non-
angular contour as compared with that species. It will be noted also that
the ambulacra are narrower, more flexuous (near the ambitus), and sunk
in much shallower grooves-than in H. elegans. The madreporite is smaller
than in H. elegans- or in Macraster texanus Roemer.3 No fascioles are
visible. In longitudinal section H. elegans is much taller, straight-sided
and less evenly rounded posteriorly than E. aguilerae, and its inter-ambul-
acral areas, including the median posterior keel more elevated. In the
individual at hand the periproct is situated lower than in material of
H. elegans collected in the Fort Worth limestone at Fort Worth, but higher
than in examples figured by Clark,4 and the anterior notch is deeper than
in Clark's figures but shallower than in some material collected by me.
'Univ. Texas Bull. 1945, pi. 8, fig. 3.
"Compare Clark, in Clark and Twitchell: U. S. G. S. Mon. LIV, pi. XL1II.
3B6se: Inst. Geol. Mex. Bol. 25, pi. XLVIII, figs. 1-3, 5.
'Clark, ibid., pi. XLII, fig. 1-4.
110 University of Texas Bulletin
It is evident that the group of Hemiaster elegans of the Fort Worth lime-
stone is in an unsatisfactory taxonomic condition and contains more than
one species.
The other individual of Epiaster aguilerae is smaller but similar in
proportions to the one figured here. Like it also, the widest point is
just anterior to the apical system and the contour is rounded; the form
of the test is longer and somewhat more pointed posteriorly. The long-
itudinal section is essentially the same. The periproct is situated higher
and is perceptibly taller and less rounded, being pointed at both ends.
HORIZON: Basal Fort Worth limestone.
LOCALITY : Subdivision 5 of Cerro de Muleros ; Individual 1, one-half
mile east of Texas Christian University, Fort Worth, Texas, locality 406.
Individual 2, one-half mile southeast of Mt. Olivet Cemetery, Fort
Worth, Texas, lower 10 feet of Fort Worth limestone.
EPIASTER SUBOBESUS n. sp.
PI. 11, fig. 3
MEASUREMENTS : Length, 89 mm. ; Width, 78 mm. ; Height, 52 mm.
HORIZON : Top five feet of Weno formation, marl facies ; Pawpaw
formation, marl facies.
TYPE LOCALITY: 720, top of Weno limestone, one mile southeast
of Riovista, Texas.
DESCRIPTION : Test rotund, elevated, tapering posteriorly to a very
narrow tall truncation sloping forwards at the bottom in the top of which
the very small periproct is located. Contour same as E. wenoensis except
more prolonged posteriorly; form straighter sided, much more elevated
than that species, apical system proportionately farther forward. Base
nearly flat, slightly raised on the posterior mid-line, but much less than in
E. wenoensis, excavated for the peristome. Ambulacra straight, arranged
as in E. wenoensis, inter-ambulacral areas notably more elevated. Un-
paired ambulacrum with about 60 similar slit-like pore pairs obliquely set.
Antero-laterals very long, with 90 or more pore pairs in each zone; all
pores equal and similar ; postero-laterals with 80 or more pore pairs, equal
similar slits. Peristome medium, transversely oval, 6.5x6.0 mm. ; periproct
extremely small, circular, 3.5 mm. diameter, much smaller and situated
relatively lower than in E. wenoensis. The description applies to the type
individual. This species might be taken as an old individual of E. weno-
ensis, but this is precluded by the differences cited above. The species
having this characteristic size and form, is common in North Texas.
Weno and Pawpaw Formations 111
ENALLASTER
The genus Enallaster ranges from the Neocomian to the Turonian, but
is especially abundant in the subtropical Cenomanian seas, where its great
development and exuberance of closely related species constitute a special
and complicated problem. The littoral deposits of the Mediterranean and
the Texas regions contain a sequence of poorly defined Enallasters, in which
the separate species are probably closely restricted in vertical range and on
careful study will prove to have great stratigraphic value; the two areas
mentioned have closely similar species.
Enallaster differs from Holaster and Stenonia in having the ambulacra!
pores sunk in ambulacral grooves instead of being flush with the surface ;
it differs from Hemiaster and Epiaster in the exceptional depth of the
anterior unpaired ambulacral groove and in the arrangement and length
of the pore zones of the unpaired ambulacrum whose pore pairs are of
alternate sizes instead of equal. Enallasters are of very diverse form,
one group being flattened and short-ovoid, one group depressed but very
elongate, and a third group rather tall and of elliptical contour.
As defined by Cotteau, Enallaster contains only species in which the
anterior unpaired ambulacrum contains alternate long and short pore
pairs. Hemiaster differs from Enallaster in having the pore pairs of the
unpaired ambulacrum slit-like and similar, and the pores of a pair sepa-
rated by a rounded tubercle. The Texas species of Hemiaster are diverse
and fall into two general groups.
A. Postero-laterals very short, biconvex, apical system placed far back
on test ; anterior row of antero-laterals with pairs of minute circular pores,
form low, with long anterior slope.
H. longisulcus (Adkins and Winton)1.
H. riovistae Adkins.
B. Postero-laterals long, more nearly straight, apical system nearly
central ; anterior zone of antero-laterals with larger slit-like pores ; form
more elevated and inflated.
H. calvini Clark.
H. elegans Shumard^
H. whitei Clark.
H. sp. (Goodland limestone).
H. comanchei Clark.
Erroneously referred .to the genus Enallaster.
112 University of Texas Bulletin
ENALLASTER WENOENSIS n. sp.
PL 5, figs. 3
MEASUREMENTS : I
(Type)
Length 25.0 mm.
Breadth 23.4 mm.
Height 14.3 mm.
Length from apical system to posterior border 9.0 mm.
HORIZON : Upper five feet of Weno formation, marl facies. Base of
Weno: base of Pawpaw clay.
LOCALITY : 720 (type locality) , one mile southeast of Riovista, Texas,
and one-half mile east of the Waco road ; 602, 618, near Fort Worth, Texas.
DESCRIPTION— TEST : Test oval in general outline, broadest point
anterior to the center, less elongate and more abruptly truncated poster-
iorly than H. riovistae n. sp. : anterior notch more pronounced than in
that species and anterior groove shorter. Apical system located a little
less than two-thirds the way back on the mid-line. The outline of the
test seen from above is ovate, with angulations ; the anterior corners of the
test are broadly round to the notch of the anterior sulcus, the posterior
corners on the ambitus are abruptly rounded to the excavated periproct
area. Oval surface inflated medially, the most prominent point being on
the mid-line about two-thirds the way from the anterior end of the test.
Aborally the highest point of the test is on the carina midway between the
posterior ends of the short postero-lateral ambulacra and the test slopes
gently anteriorly from this point, as in E. bravoensis Bose, and H. riovistae.
Anterior unpaired ambulacrum sunk in the deep anterior sulcus which
is relatively shorter and narrower than that of H. riovistae n. sp.
Each zone has about 31 pairs of ambulacral pores. About the first
twelve pore pairs are short, similar and equal except that they increase in
size from the apical system anteriorly. They have each two equal short
slits separated by a tubercle. Next come five pore pairs, three long and
two short, alternating. Next come two groups of two short pairs each,
alternating with long pairs. Thereafter anteriorly the pores are short and
similar. Throughout this series in all the short pairs, the pores of a
pair are separated by a tubercle, which in all the long pairs is lacking.
The type agrees with this description. The narrow ambulacral plates,
reaching the mid-line, have each two transverse rows of variable sized
tubercles, irregularly arranged.
Weno and Pawpaw Formations 113
Anterolateral ambulacra: Diverge from apical system at angle of 180
degrees, then turn forward, their middle parts making, if produced, an
angle of about 45 degrees with each other ; then turn laterally and cross
the ambitus at a point posterior to the anterior corner of the test. The
anterior pore zone has 18 to 20 small, circular, closely spaced pore pairs.
The posterior zone has about 27 pairs of slit-like pores, the anterior pore
being much shorter.
Posterolateral ambulacra: Short, inflated centrally diverge at angle of
about 130 degrees from each other. Each zone has about 12 pore pairs,
those of the posterior zone being more elongate than those of the anterior
zone. In each zone the anterior pore is shorter than the posterior.
Apical system: Four genital plates, their conspicuous thick-lipped per-
forations making the four corners of a square. Oculars small, perforated.
Peristome: Ovoid, depressed, posterior lip straight, with an elevated
median carina behind it.
Periproct: Ovoid, inferior margin extended downward; situated at top
of vertically excavated area in posterior truncated area.
This species is most similar to E. bravoensis Bose, from which it differs
in many particulars. E. bravoensis in form resembles E. texanus (Roe-
mer) and is the inflated texanus-like species which is widespread in the
upper Washita and which has been so frequently mistaken for E. texanus.
We have examples of it from the Weno to the Grayson formations, and it
has been found in the Buda limestone (Whitney) . E. bravoensis is not so
tall as E. texanus and is not therefore so inflated as. that species ; yet it
is more rotund than E. wenoensis* and lacks the angular contour of this
species. E. wenoensis is more ovate in form and does not have the long
posterior narrowing of the test seen in many individuals of E. bravoensis.
It is abruptly narrowed posteriorly and has a truncate posterior end.
There is variation in the figured material of E. bravoensis in this regard,
and in the absence of a designated type individual it is impossible to say
which condition is typical for that species. Bose's plate XLI, figure 5,
shows an individual in which the posterior narrowing is slight and the
truncation is broad, as in E. texanus or E. mexicanus; in plate XLII,
figure 9, the narrowing is prolonged and the truncation narrow, as in
E. wenoensis. However, a constant and distinctive feature of E. weno-
ensis is that the posterior end of the test is not merely truncate but is
deeply excavated vertically, and in this excavation the periproct lies. In
E. bravoensis as figured, the apical system is subcentral or at least far-
ther forward than in E. wenoensis; the main limits of the antero-laterals
therefore diverge at a wider angle (about 80 degrees) in E. bravoensis;
114 University of Texas Bulletin
and this position of the apical system is to some extent correlated with
the elongation of the test. The anterior ambital notch in E. wenoensis
is always sharper and deeper than in E. bravoensis; in the latter species
it has the same form as in H. riovistae here described, while in this respect
E. wenoensis and H. longisulcus (Adkins and Winton) are closely similar
to each other. In E. wenoensis there is a conspicuous high point on the
median .carina halfway between the apical system and the posterior end
of the test; in E. bravoensis and H. riovistae the carina is low and the
highest point is variable, often lying near the apical system. E. bravoensis
in addition has a distinctly angular inferior inflation to the test which
in our species is evenly rounded.
ENALLASTER BRAVOENSIS Bose
PI. 8, fig. 4
1910: Enallaster bravoensis Bose, Inst. Geol. Mex., Bol. 25, p. 168, pi. 41, figs. 5-10;
pi. 42, figs. 2-12; pi. 43, figs. 1-2, 6-7.
1916: Enallaster bravoensis Whitney, Bull. Amer. Pal. No. 26, p. 16, pi. 6, figs. 3-5.
1920: Enallaster bravoensis Adkins and Winton, Univ. Texas Bull. 1945, p 58 pi 9
fig. 11.
This species is occasional in the Upper Washita formations, Weno to
Buda, and in North Ttexas is still unknown from the lower formations.
At Cerro de Muleros it is reported from subdivisions 5, 6, and 8 (Fort
Worth to Grayson). This species differs from Enallaster wenoensis, which
also is truncated and tapering posteriorly, by its more elevated and in-
flated form, smaller depth of ambulacral grooves, and its taller and dif-
ferently shaped longitudinal section in which the anterior slope is shorter,
more abrupt and more rounded.
ENALLASTER sp. aff. TEXANUS (Roemer)
There are in the Upper Washita formations undefined species similar
in form to Enallaster texanus (Roemer). These are abundant in the
Weno and Grayson marls, and are in need of study and revision.
HEMIASTER CALVINI Clark
PI. 5, figs. 1, 2, 4; PL 6, fig. 3; PI. 8, fig. 6
This species may be recognized by its tall rounded form and its short,
deep ambulacral grooves. It is somewhat variable in form and size, but
Weno and Pawpaw Formations 115
the most common variants are here figured.
Form elevated ; outline angular, broadly truncated and shallowly ex-
cavated posteriorly, with a shallow anterior ambital notch, widest just
posterior to the antero-lateral ambulacra. The apical system is a little
posterior to the center of the test, the distances in front of and behind it
having the ratio 10:8. Ambulacra deeply excavated, the unpaired one
being longest; the antero-laterals are longer than the postero-laterals (ra-
tio 9:7) ; the antero-laterals diverge at an angle of about 105 degrees, the
postero-laterals at about 45 degrees. The unpaired ambulacrum is slightly
wider than the others. The posterior median keel and the interambulacral
areas are elevated, the former being sharp-topped. Peripetalous fascicle
visible but irregular. Pores of unpaired ambulacrum short, slit like,
oblique, separated by a prominent tubercle. Pores of lateral ambulacra
elongate transverse slits which are nearly equal in the forward and the
rear zones. Peristome elongated transversely, with a prominent thick-
ened posterior lip; periproct high, vertically elongate, ovate. The longi-
tudinal section is distinctly elevated, posterior slope straight and inclined,
anterior slope rounded, the highest point of the test being on the posterior
median keel just back of the apical system.
HORIZON: Weno to Buda formations.
The Weno marl contains another species which has deeply excavated
short ambulacra, much constricted at each end and flared in the middle.
These ambulacra are remarkably short and inflated and have a very
characteristic appearance. The whole ambulacral system is placed for-
wards on the test, the posterior median keel and the interambulacral areas
are elevated, she outline is almost circular and non-angular, the form
is low, and the anterior median notch is shallow.
This species has some resemblance to the poorly figured and described
species Hemiaster bexari Clark.
HEMIASTER RIOVISTAE n. sp.
PI. 6, fig. 4; PI. 8, figs. 2-3,5
MEASUREMENTS : (Type)
Length on mid-line 25.5
Width 23.5
Height 14.0
HORIZON: Top of Weno formation, marl facies.
LOCALITY: 720 (type locality), one mile southeast of Riovista,
Texas, and one-half mile east of the Waco road.
116 University of Texas Bulletin
DESCRIPTION— Test: This species has nearly the form of Enallaster
bravoensis Bose, but differs in many respects, notably in having the pore
pairs of the unpaired ambulacrum all similar. Test low, elliptical in gen-
eral outline, notched at the anterior ambitus, rounded laterally, with three
distinct angulations, broadly truncate posteriorly. Anterior sulcus long,
apical system situated slightly more than two-thirds the length of the
mid-line from the notch of the anterior sulcus. Highest point of test on
the low posterior median carina about one-fifth the length of the test from
the posterior end. From this point the mid-line curves sharply poster-
iorly to the top of the truncated posterior end. This point is only slightly
taller than the edges of the anterior sulcus just in front of the apical
system. Slope of test forward from apical system gentle, almost a
straight line, similar to that of E. bravoensis Bose. The middle is the
most inflated point on the test. Inferiorly the most prominent point is
on the mid-line three-fourths the way back from the anterior end ; the shell
therefore is tallest at this point and anteriorly is wedge-shaped, as in
E. bravoensis Bose. There is an elevated median tuberculated area and
the peristome lies in a deep depression of the recurved anterior sulcus and
is bounded posteriorly by an overhanging pointed lip. Margins of shell
sharply rounded on approaching ambitus, and coarsely tuberculate.
Around each tubercle is a circlet of small tubercles, and the intervening
spaces recovered by- fine granules irregularly scattered. Oval projections
of postero-lateral ambulacra consisting of large smooth elongate plates
with scattered tubercles and fine granules. Laterally the test bears sev-
eral fascicle-like bands each consisting of three crowded rows of the
smallest sized granules.
Anterior unpaired ambulacrum: Long, shallow, sides nearly straight,
making a rather shallow notch at the ambitus. Each pore zone has about
32 pairs of transverse slit-like pores, the pores of a pair being separated
by a conspicuously elevated, transversely elongate tubercle. The pores are
similar and the ten nearest the apical system show a graduation in size;
the others are approximately equal, except near the ambitus, where they
are more nearly circular. The pore pairs lie each on an elongate ambul-
acral plate which reaches the middle. Each plate has a double row of
small granules.
Antero-lateral Ambulacra: Diverge at an angle of 180 degrees and
turn forward making over the central part of their course an angle of
about 47 degrees with each other. They then diverge and cross the am-
bitus far anteriorly. The anterior pore zone consists of about 22 pores
of minute, closely spaced, circular pores, situated for the most part about
Weno and Pawpaw Formations 1J7
the diameter of a pore apart. These are situated in the antero-median
quadrant of a quadrate or trapezoidal ambulacral plate which bears two
or three large tubercles. The posterior zone consists of about 32 pairs,
each having an anterior oval pore and a posterior wedge-shaped slit nar-
rowest at the forward end.
Postero-lateral ambulacra: Short, rather wide and bulging in the cen-
ter, axes straight diverging at an angle of about 115 degrees from each
other. The anterior zone has about 12 pairs of short slits; the posterior
about 14 pairs of nearly equal longer slightly oblique slits. All of these
pores decrease in size toward each end of the zones.
Apical system: Four genital plates, the right anterior one being the
elongated madreporite, the posterior pair slightly farther apart than the
anterior pair ; four perforated oculars.
Peristome: Transversely oval with a slightly emarginate lip. The lip
posteriorly is elevated into a blunt high tip or carina.
Periproct: In shape an oval, transversely situated but with the rounded
inferior margin slightly bulged downward; each diameter (on the type)
about 2.8 mm., situated high on posterior truncated surface two-thirds the
way up.
Aside from generic characters the following differences will assist in
separating H. riovistae n. sp. from Enallaster wenoensis n. sp. E. weno-
ensis has the apical system farther forward; the antero-laterals diverge
at a slightly greater angle ; the anterior ambital notch is deeper and more
sharply incised; the form is broader, less elongate, more nearly circular,
distinctly less flat and more constricted posteriorly. The area in which
the periproct lies is not merely truncate, but is sharply excavated giving
a narrow vertical groove, while in H. riovistae the posterior end of the
test is broadly truncate and the excavation is broad and shallow; and the
pores of the anterior unpaired ambulacrum are in part alternating long
and short pairs, instead of being all similar and separated by a tubercle
as in H. riovistae. The more posterior position of the apical system of
H. riovistae results in its having a longer anterior sulcus, it being inter-
mediate in this respect between E. wenoensis and H. longisulcus. The an-
tero-laterals are in many individuals which are here referred to E. weno-
ensis much more sunken than in H. riovistae. The only other described
species with which H. riovistae might be confused is E. bravoensis which
has long and short pore pairs in the anterior unpaired ambulacrum instead
of having all the pore pairs similar. H. longisulcus (Adkins and Winton)
has these pore pairs similar, but it is at once distinguished by its lower,
more elongate form, and by the unusually long anterior sulcus and the con-
sequent posterior position of the apical system.
118 University of Texas Bulletin
PELECYPODA
NUCULA NOKONIS n. sp.
PI. 10, figs. 12-16, 19-20
MEASUREMENTS : I
Length 17.0 mm.
Height 13.4 mm.
Thickness 8.3 mm.
HORIZON : Blue shale and red clay-ironstones of upper half of Weno
formation, Red River region.
LOCALITY : 601, pit of brickyards, one and three-fourths miles south-
east of Gainesville, Texas (type locality) ; 604, cut of Frisco track, three-
fourths mile north of Union Station, Denison, Texas.
DESCRIPTION : Shell inequilateral, sub-equivalved, 'sub-triangular in
contour, with fine radial ribs.
Right valve, exterior: Beak sharply rounded, angle 100 degrees; a
straight rounded ridge runs from the umbo to the anterior angle, making
with the anterior margin a long low triangle* whose other two sides are
almost straight portions of the anterior margin. These portions are in
length as two to one, the dorsalmost portion being the lunger, and make
with each other an angle of 15 degrees. The ventralward portion, if ex-
tended, would make with the extended ventral side an anterior angle of
60 degrees; the actual angle is sharply rounded. The ventral margin is
gently convex downward, and extends backward to the sharply rounded
posterior angle (90 degrees). The postero-dorsal margin is straight.
The ornamentation consists of about 47 very flat low radial ribs which
are unbranched and continuous from beak to ventral margin. Between
these lie fine straight depressions one-sixth to one-eighth the width of a
rib. The ribs are crossed by fine scalloped growth lines with the convex-
ities pointed ventrally, giving to the growth lines a fine crenulate appear-
ance. On the anterior area (lunule) the ribs disappear and the growth
lines thicken slightly. This area contains a radial anterior ridge and a
concurrent posterior depression ; the growth lines in crossing these are
crenulate. TWO deeper concentric constrictions representing stages of
growth lie in the ventral half of the valve.
On the shorter posterior area (escutcheon) the growth lines turn dor-
sally and passing over a radial depression and a radial ridge, converge to
the margin.
Right valve, interior: The rounded, posteriorly directed beak is slightly
elevated over the posterior margin. This margin is gently convex over
Weno and Pawpaw Formations 119
its dorsal three-fifths and bears a taxodont series of nine teeth of which
the two dorsalmost and the one ventralmost are shorter and narrower
than the others. The antero-ventral two-fifths of the margin is concave
and lies just posterior to the truncately elliptical scar of the post-adductor
muscle. The posterior end of this margin is the posterior angle, from
which the rounded ventral margin runs to the anterior angle. This margin
is more sharply rounded near the posterior angle. The antero-dorsal mar-
gin is distinctly bulged, and its dorsal two-thirds bears a taxodont series
of twenty teeth, which taper in size at each end.
Beneath the umbo is a narrow triangular pit directed downward and
anteriorly; and posterior to it is a parallel tooth containing along its
length, except at the top, a sulcate depression.
Left valve, exterior: The beak is rounded and forms an angle of about
105 degrees. The posterior area is contained between the straight post-
erior margin and a curved ridge which is the arc of a circle. In this area
the growth lines turn sharply dorsally and converge at the margin. In
its center is a radial elevation on whose outer surface are irregular crenu-
lations which are oblique to the growth lines and continuous with those on
the main portion of the valve. Lateral to the elevation is a concurrent
depression and dorsal to it a small plane area. The posterior angle is
100 degrees. The ventral margin is curved ; and more sharply so at the
posterior end. The anterior area is a triangular space included between
the convex anterior margin and a concurrent but divergent ridge which
runs from the beak to the anterior angle. It bears numerous^ coarse
crenulations which are continuous with those over the main body of the
valve.
The ornamentation of the valve consists of numerous radial simple flat
ribs similar to those of the right valve; and concentric depressions and
growth lines. The two valves fit together evenly with a slight ventral
gape.
Left valve, interior: This valve is essentially similar to the right valve.
Anterior to the beak and ventro-lateral to the taxodont series of teeth
is an elongate tooth pointed antero-ventrally and fitting into a socket in
the right valve. Its end lies below the tenth tooth anterior to the beak.
Type individual: This description is compiled from three individual?
of which the first, showing the exterior of the right and left valves, is
to be considered the type individual. It and the other two, as many of
the other individuals, were found in the blue marl of the upper half of
the Weno formation, 20 feet below Quarry limestone in cut of Frisco track,
one mile north of Union Station, Denison, Texas (604).
120 University of Texas Bulletin
NUCULA WENOENSIS n. »p.
PI. 10, figs. 10-11
MEASUREMENTS: I (type) II III
Breadth 8.5 10.2 13.0
Height 14.9 17.5 18.5
Length 20.5 23.7 26.0
HORIZON : Weno formation, blue shale, Red River region, occasional ;
clay ironstone, occasional.
LOCALITY: 604, Frisco cut, three-fourths mile north of Union Sta-
tion, Denison, Texas (type locality) ; 601, pit of brickyard, one and three-
fourth miles southeast of Gainesville, Texas.
DESCRIPTION: Shell sub-equivalved, moderately inflated, inequi-
lateral, beaks placed back of the middle of the valve. Ventral margin a
long, sub-elliptical curve, sharply angulated posteriorly, more rounded an-
teriorly. Anterior margin long, slightly convexed, beaks opposite, approx-
imate; posterior margin shorter than anterior, nearly straight, lacking
a prominent incision just posterior to the beaks. Anterior areas cres-
centic, together forming an elongate biconvex strip, posterior areas form-
ing a strip proportionately shorter but equally wide. These are crossed
by plain recurved growth lines.
Valves nearly smooth in appearance; ornamentation consists of numer-
ous fine. simple radial s^riaeiform ridges, crossed by growth lines and
growth rings. These ridges on reaching the ventral border form a slightly
incised, non-crenulate edge. Hinge taxodont, essentially as in Nucula
nokonis.
This species differs from N. hokonis in its form and ornamentation.
The anterior margin 'is straighter and longer; the posterior margin is
straighter and lacks the sharp notch just back of the beaks, having in-
stead a gentle curvature ; the posterior "areas" are much more pronounced
in side view, and instead of lying flat are elevated at the line of junction
of the valves by a posterior projecting carina. The ornamentation at once
distinguishes the two species, for in N. nokonis the radial ribs are very-
pronounced and the concentric growth lines on crossing them form a
system of prominent squares ; the concentric ribs on approaching the an-
terior border become zigzag or wavy making a conspicuous V-shaped an-
gulation, and in the same region the concentric ribs become crenulate and
lamellated. The radial ribs form a prominent scalloped edge at the ven-
tral margin of the valve.
Weno aud Pawpaw Formations 121
ARCA WASHITAENSIS n. »p
PI. 10, fig. 6
MEASUREMENTS : I (type) II III IV V
Length 9.2 12.6 8.1 6.7 8.0
Height 7.0 9.5 5.0 '4.9 6.2
Thickness 6.6 9.5 5.6 4.6 6.4
<• Length of -hinge line 7.3 9.9 6.8 5.7 7.0
HORIZON: Pawpaw formation, clay faciea, widely distributed, John-
son to Denton counties ; ironstone and sandstone f acies, widely distributed,
Denton County to east of Bennington, Oklahoma. A similar, and prob-
ably identical species of Area occurs in the Grayson marl and clay at
Burleson and Roanoke, Texas; in the Denton clay at Denison, Texas; and
in the Duck Creek marl, Grayson to Johnson counties, Texas.
LOCALITIES: 714, near Fort Worth, Texas (type locality), all Paw-
paw localities in the Fort Worth region. This fossil is found wherever
Pawpaw fossils occur, in Denton, Tarrant and Johnson counties, and
practically so in the Red River region. Its zone of abundance is one of
the most reliable markers of the Pawpaw formation.
DESCRIPTION: Shell small, valves very inflated, subequal inequi-
lateral, taller posteriorly than anteriorly. Beaks prominent, remote, pro-
jecting, rounded, situated slightly anterior to the center of the shell. An-
tero-dorsal margin short, concaved; posterior margin longer and nearly
straight. Anterior margin short, sharply rounded, ventral margin long
and nearly elliptical, dorsal margin broadly rounded. Hinge line long
and straight and marked by a crenulated thin ridge in casts of the in-
terior. The shell gapes slightly at its posterior end. The valves are orna-
mented by numerous low, fine, subequal radiating striae, which equal in
width the valleys between them ; and a few (7 or more) unequal, coarse
concentric ridges lying mainly on the ventral half of the valve.
This Area may be distinguished from others described from the Texas
Comanchean strata by its form and size. It is a very characteristic pyrite
and hematite fossil and is widespread geographically in the Pawpaw form-
ation, and in addition appears to have considerable vertical range, reap-
pearing in the Upper Washita in association with pyritic Engonoceras,
Turrilites, Hamites, Scaphites and starfishes with each invasion of the
clay and ironstone phase of deposition.
122 University of Texas Bulletin
GERVILLIOPSIS INVAGINATA (White)
1888: Dalliconcha invaginata White, Proc. Acad, Nat. Sci., Phila., p. 35, pi. 2, figs. 4-5.
1889: Gervilliopsis invaginata Hill: Geol. Surv. Texas Bull. 4, p. 9.
1896: Gervilliopsis invaginata Stanton and Vaughan, Am. Journ. Sci., IV series, vol. 1,
vol. 1, pp. 21-26.
1910 : GervUleia invaginata Bose, Inst. Geol. Mex., Bol. 25, p. 87.
1920: Gervilliopsis invaginata Adkins and Winton, Univ. Texas Bull. 1945, p. 67, pi. 18,
fig. 1.
This shell abounds in the lower Weno of Cooke County, where on fresh
exposures it is found with the nacreous shell intact. It has a restricted
vertical range and is a reliable marker for the basal Weno north of the
Brazos River. It has not been reported from South Central Texas.
Stanton and Vaughan, however, record the species from subdivision 6
(Weno-Pawpaw) of Cerro de Muleros.
OSTREA CARINATA? Lamarck
The known distribution of carmata-like species in Texas has already
been published.1 Pervinquiere- has figured types of Ostrea carinata Lam-
arck ; and Texas material is now being assembled for a critical study and
comparison with related European material. Oysters of the group of
0. carinata and widespread in North, Central and West Texas at different
stratigraphic levels, and among them a zone of abundance of the smaller
forms in the upper part of the Weno limestone (Quarry group of North
Texas) and a scattering representation in the Pawpaw formation.
OSTREA sp. aff. DILUVIANA Linnaeus
There are in the Weno and Pawpaw formations three oysters with zig-
zag coarse margins and ribbed valves, resembling the group of Ostrea
diluviana. One of these occurs in the Weno and Mainstreet limestones
and is similar to that figured by Hill from the Austin Chalk (U. S. G. S..
21st Ann. Kept., pt. 7, pi. XLV, fig. 2). Another species from the Weno
marl is smaller and thinner, and the margins are crenulate (Univ. Texas
Bull. 1945, pi. 16, fig. 1). A third unfigured species from the Weno marl
has few prominent zigzag ribs of varying height. These species will likely
be found to have considerable vertical range.
1 Winton and Adkins, Univ, Texas Bull. 1931, p. 57; Adkins and Winton, Univ. Texas
Bull. 1945, p. 59.
2Pervinquiere, Pal. Univ., 3 me ser., 1910, fiches 197-198.
Weno and Pawpaw Formations 123
OSTREA (ALECTRYONIA) QUADRIPLICATA Shumard
1860: Ostrea quadriplicata Shumard, Trans. St. Louis Acad. Sci., vol. 1, p. 608.
1879: Ostrea quadriplicata White, llth Ann. Kept. U. S. G. and G. Surv., Terr., pp. 275-
276, pi. 5, fig. 6a.
1920: Ostrea quadriplicata Adkins and Winton, Univ. Texas Bull. 1945, p. 60, pi. 16,
figs. 6-10.
This species has not been seen above the Mainstreet limestone, where
it is rare, or below the Denton marl. It is abundant at the top of the
Denton marl, with Ostrea carinata and Gryphea washitaensis ; and at the
Weno-Pawpaw contact in the Quarry limestone, with Ostrea carinata.
Gryphea washitaensis and cidarid spines.
This species is not known in South Central Texas, but is abundant near
El Paso in subdivision 6 (equivalent of Weno-Pawpaw).
EXOGYRA sp. off. ARIETINA Roemer
A small species of Exogyra, juvenile and young adult stages, was found
in the basal Weno at locality 611, near Fort Worth, Texas. The evolution
of the arietina group leaves large gaps to be filled in ; the group is known
from the Goodland limestone, upper third, and the Kiamitia marl (E. spp.
aff. plexa, ribbed and non-ribbed), from the Duck Creek limestone (E.
plexa) ; the Mainstreet limestone (E. arietina) and the Grayson marl (two
species aff. E. arietina).
PECTEN INCONSPICUUS Cragin
PI. 11, fig. 4
1895: Pecten inconspicuus Cragin, Colo. Coll. Stud. 5, 1894 (1895), p. 61.
Cragin's description follows:
"Shell small, thin, subcircular, a trifle higher than long, slightly trun-
cated anteriorly and posteriorly, right valve gently convex, its outer sur-
face smooth except for faint concentric striae and a few remote, subim-
bricate growth-lines; umbonal angle sharp at apex, nearly a right angle;
anterior ear (imperfect in the type) re-entrant below, as indicated by the
direction of the striae upon it, outline of posterior ear marking an obtuse
angle, its posterior margin rather more than one and a half times as long
as its dorsal. Left valve unknown.
"MEASUREMENTS : Height 9.5, length 8.75, convexity of left valve
1 mm.
124 University of Texas Bulletin
"OCCURRENCE : On slope of Pawpaw Creek,'east of Denison, Texas,
in red ochraceous shell-conglomerate of the Pawpaw clays. The associate
fossils are Ostrea quadriplicata, Tapes dentonensis, Yoldia microdonta
Turritella seriatim-granulata, Sphenodiscus, Turrilites, etc."
Although Cragin's description is very brief and general, it fits a common
Weno species of Pecten in many respects; the locality also makes it prob-
able that our Gainesville and Denison material is to be referred to Cragin's
species.1
HORIZON: Ironstone and shale facies, upper two-thirds of the Weno
formation. Basal Pawpaw formation, sand-ironstone facies. Very rare
south of the Red River region.
"LOCALITY: Cut of St. Louis and San Francisco Railway, one mile
north of Denison, Texas (PI. 11, fig. 1) and pit of brickyards, one and
three-fourths miles east of Gainesville, Texas. Numerous localities in
Cooke and Grayson counties, Texas. In the pit of the Gainesville brick-
yard there are extensive sheets of nacreous shells consisting largely of
Pecten inconspicuus, Gervilliopsis invaginata and prodissoconchs and later
embryonic stages of Gryphea washitaensis.
DESCRIPTION : Shell slightly elevated, smooth, jnequivalve, inequi-
lateral ; ventral margin almost the. arc of a circle whose diameter is the
antero-posterior dimension of the shell. Antero-dorsal margin almost
straight, postero-dorsal margin slightly concave near middle and more
elevated by a sharp fold above the ear than the antero-dorsal margin •
the two make an angle of about 95 degrees at the umbo, the angle being
pointed and very slightly rounded at the tip ; the angle made by lines drawn
from the extremities of the two margins to the umbo is about a right
angle. The umbo projects slightly over the hinge line. Anterior and
posterior ears triangular, the latter having a longer base along the margin
than the former, and having nearly twice the area. Hinge line straight,
making an angle of about 46 degrees with the antero-dorsal margin and
an angle of about 42 degrees with the postero-dorsal margin. The term-
inal angle of the anterior ear is about 95 degrees; of the posterior ear,
about 100 degrees. The latter angle is broadly rounded.
The ears have fine parallel sigmoid growth line which bend toward the
umbo at the hinge line, but at the dorsal margin bend anteriorly and
posteriorly and after ascending these margins, course concentrically across
'This species has never been figured, so far as I can discover; the type is presumably
in the Colorado College museum, but efforts to get information about it have been
misspent.
Weno and Pawpaw Formations 125
the valve. The growth lines on the valve are fine but unequal; there are
also irregular coarser, more widely spaced imbricated rings.
In addition, the right valve and its ears are ornamented with numerous
fine striaeiform radial curved elevated costellae which spread fan-wise
as they approach the margin; these are irregularly truncated near the
ventral margin, and on the ears, by intersection with the coarser radial
striae, form a network of small squares.
The left valve is apparently slightly concave and has a similar structure
to the right valve.
PECTEN GEORGETOWNENSIS (Kniker)
1919: Neithea georgetownensis Kniker, Comanchean and Cretaceous Penctinidae of
Texas. Univ. Texas Bull. 1817, p. 31, pi. VI, figs. 1-3.
1920: Pecten georgetownensis Winton and Adkins, Geology of Tarrant County, Univ,
Texas Bull. 1931, pp. 22, 64, 66.
1920 : Pecten georgetownensis Adkins and Winton, Univ. Texas Bull. 1945, p. 70, pi. 12,
figs. 5-6.
This species may be distinguished by its form and by the radial grooves
located on the center of the primary and secondary ribs of the right or
both valves. These grooves, however, occur sporadically on other species
of Pecten of the P. subalpinus type. It marks the basal third of the Weno
formation, marl facies, and is associated with Turritella worthensis,
Ancycloceras bendirei, Remondia acuminata Cragin, Pedinopsis symmetrica
Cragin, and numerous widely ranging species. It is widespread and abund-
ant.
VENERICARDIA WENOENSIS n. .P.
PI. 6, fig. 2
MEASUREMENTS (type individual) :
Antero-posterior 23 mm.
Dorso-ventral . 23 mm.
Right-left 18 mm.
HORIZON AND LOCALITY: Basal Weno formation, marl facies,
locality 618, near Fort Worth, Texas (type locality) ; middle Weno shales,
"buff marl," below the main GerviUiopsis invaginata zone, locality 601,
near Gainesville, Texas.
DESCRIPTION : This Venericardia somewhat resembles V. alticostata
Conrad var.: of the Eocene, but has the ribs more strongly imbricated
126 University of Texas Bulletin
and the ventral margin less nearly circular.1 I know of no other similar
species from the Comanchean.
Shell oblique, elliptical in outline except for the projecting, elevated
umbonal region. Beaks greatly recurved. Ventral margin almost an el-
lipse, sharply curved below the beak, gently curved behind ; dorsal-posterior
margin nearly straight. The valves have about 24 sharply raised ribs,
which bear remote but unevenly spaced, elevated, nodose imbrications.
The lateral dimension of the shell is thick, and the species varies some-
what in outline. The hinge and other interior details are unknown.
PROTOCARDIA »p. aff. MULTISTRIATA (Shumard)
PI. 10, figs. 21-26, 32
This beautiful Protocardia occurs as casts and molds in the clay-iron-
stone of the Gainesville brickyards and shows in nacreous preservation
the minutest details of the exterior and the interior of the shell. Most
frequently the shell has crumbled into a friable powder and falls to pieces
as the rock is broken open. It then leaves in the ironstone excellent molds
of the exterior of the shells showing the radial and concentric striations
of the exterior and the details of the hinge, and casts of the interior
showing details of the dentition, the two muscle scars, pallial line, etc.
Frequently the shell has been removed by weathering and the ironstone
carries a > cavity of its exact shape bounded by the cast and the mold.
Rarely in the ironstone but usually in the blue shale, the original shell
is preserved intact.
The Protocardia group of the Texas Comanchean has not been satis-
factorily studied and its species are still poorly defined. As in many
other Texas genera this uncertainty can be resolved only by a critical
description and photographic illustration of the types. Here as in other
genera where new species might have been founded, this has not been
done pending a better understanding of the relations of the species already
described.
Shell inequivalve, inequilateral, biconvex, ornamented with sixteen or
more serrate radial lines and about 75 round topped subequal concentric
ribs separated by narrow valleys. The dorsal margin of the shell is
arcuate interiorly, and anteriorly is more thickened. It bears several im-
bricated lamellae parallel to and below the hinge line. The region under
the beak is deeply excavated.
'Harris, The Midway Stage, Bull. Amer. Pal., 4, pi. 4, flg. 12. 1896; and, The Lignitic
Stage, Bull. Amer. Pal., 9, pi. 11, fig. 1, 1897.
Weno and Pawpaw Formations 127
HORIZON : Middle and Upper Weno shale and clay-ironstone.
Locality of figured material : 604, cut of St. Louis and San Francisco
track,- three-fourths mile north of the Union Station, Denison, Texas ; the
species occurs throughout the Red River region, and is abundant at locality
601, pit of brickyards, near Gainesville, Texas.
CORBULA WENOENSIS n. .p.
PI. 10, figs. 1-4
MEASUREMENTS: I II III
Length 10.6 11.6 11.2
Breadth (one valve) __. 3.8 4.4 4.0
Height 7.7 8.1 8.0
Length of rostrum 2.0 2.5 2.5
HORIZON: Weno formation, upper half, clay and ironstone phase,
abundant; Pawpaw clay, rare. Abundant in the Red River region.
LOCALITIES: 604, near Denison, Texas (type locality); 601, near
Gainesville, Texas.
Shell small, inequivalve, concentrically ribbed with a truncated rostrum.
Right valve, exterior: Form a very irregular quadrilateral ; size small.
Viewed directly from above, the valve is roughly pear shaped and consists of
a very inflated rotund body and a narrowed and depressed posterior siphon
tube or rostrum. The umbonal margin is roughly the arc of a circle whose
diameter equals the height of the shell. This border passes by a sharp-
pointed curve of 120 degrees into the anterior border, which is almost a
straight line making an angle of about 45 degrees with the dorso-ventral
axis of the valve. The anterior border passes into the ventral border by a
sharply rounded curve which is approximately the arc of a circle one-half
the diameter of the dorso-ventral dimension (height) of the shell ; the anter-
ior and ventral borders if extended would meet at an angle of about 55 de-
grees. The ventral border is very slightly convex and this approximates
a straight line through one-half the greatest length of the shell, where it
is perpendicular to the dorso-ventral axis. A little anterior to its middle
there is slight concavity which involves the lower two or three ribs of
the shell. The ventral border now curves upward and posteriorly, reach-
ing the narrowed siphon tube.
The snout-shaped siphon tube lies opposite the middle one-third of the
height of the shell and is roughly a right angled isosceles triangle whose
hypotenuse is the line of attachment to the body of the valve. This line
of attachment is a narrow constricted or depressed zone which notches
128 University of Texas Bulletin
both the ventral and the dorsal margins of the valve and gives to the
rostrum an inflated appearance; the notch in the dorsal margin is the
deeper and more pronounced one. Posterior to the depressed zone and
running slightly divergent to it is a rounded ridge which assumes a con-
ical inflation as it approaches the postero-ventral extremity of the ros-
trum; on the rostrum dorsal to this ridge is a parallel narrow depression
and beyond it a rounded inflation which forms the postero-dorsal extrem-
ity of the rostrum.
The ornamentation consists of thickened, rounded, concentric ribbings,
which are broadly flattened on their tops and descend by almost right-
angled sides to small plane-bottomed valleys lying between them. On the
dorso-ventral axis the widths of ribbings and valleys are about as 2 to 1.
The ribs and valleys decrease in width at the anterior margin and at the
constriction of the siphonal tube.
The ventral one-half of the shell contains 12 rounded ribbings ; the dorsal
one-half contains 17 rounded ribbings of similar form but of constantly
decreasing size, and in addition in the umbonal region 25-30 fainter rib-
bings which resemble growth lines.
These 29 heavier ribbings course posteriorly making broad downward
convexities to the region of the siphon tube constriction ; their posterior
ends lie in the depressed zone mentioned. They then rise onto the elevated
ridge which lies near the anterior end of the rostrum, and course over the
inflated rostrum to its dorsal margin. On this elevated ridge the com-
ponent growth lines in the ribbings apppear as slight thin imbricated
lamellae. Not all of the ribbings run continuously from the anterior to
the posterior margin. Towards the anterior margin some of the rib-
bings, especially the dorsal ones fuse by twos into broader and more de-
pressed flat bands. The ribbings on a whole are more flattened and more
consolidated on the anterior margin, and more resolved into growth lines
on the posterior margin, in the neighborhood of the siphon-tube. In one
ribbing, splitting is seen over the middle half of the shell. In one place a
small auxiliary ribbing between two of usual size, is seen over the middle
half of the shell.
The right valve is. somewhat larger than the opening into which the
left valve fits, so that the arched, rotund margins of the right valve enclose
an elliptical basin shaped visceral space upon which the reduced left valve
lies.
Right valve, interior: Viewed directly from above, the cavity of this
valve has an elliptical contour except at the siphonal end where the mar-
gins of the ellipse are drawn out so that each margin has an inward facing
convexity ; the dorsal margin then slants ventrally and posteriorly to meet
Weno and Pawpaw Formations 129
the ventral margin. There is also a deep rounded concealed recess under
the umbo, from this viewpoint. The anterior adducter muscle scar is a
small subcircular basin-like depression with a raised rim whose dorsal
border connects with the pallial line, a faint narrow groove which ap-
proaches the ventral margin as it courses towards the post adducter scar.
This scar occupies a rounded-triangular elevated area lying between two
more elevated ridges.
The more anterior ridge is a shelf-like lamina which separates the body
cavity proper from the siphonal (rostral) extension of the shell; and as
it passes umbonally it unites with the more posterior ridge forming a
U-shaped junction and enclosing between the two ridges the scar of the
adductor muscle. The united ridge continues anteriorly as the ventral
edge of a broad excavated pit or socket. The external (prismatic) layer
of the valve forms a distinct umbonal imbrication which makes up the
dorsal edge of this socket. This inner edge of the external layer passes
anteriorly, including the umbo but excluding the tooth against which it is
apposed; and proceeds to encircle and parallel the anterior and ventral
margins of the valve as far as the ventral border of the rostrum, making
an imbricated impression about midway between the pallial line and the
ventral margin. The thick external portion is cancellated and penetrated
by irregular concentric airspaces formed by the loose apposition of long
lamellae. The external prismatic portion makes up .8 of the thickness
of the shell ; the inner portion is porcellanous and in places pearly-irides-
cent.
Rostrum: The inner layer emerges from the body cavity proper onto
the rostrum, where it is thrown into two small elevated folds which cross
each other almost at right angles and consequently form four depressed
spaces sloping away from them at either side. The shorter fold is in
the antero-posterior axes, and the longer one is continuous with the um-
bonal imbrication mentioned above.
DISCUSSION : The description of the unfigured Cragin species C. cras-
sicostata, agrees with this species in some particulars, but disagrees es-
pecially in the number of concentric ribs. In Cragin's Kansas material
this number is "7 or 8 on the basal half of a shell the same number of
millimeters high," while in our material the number is 11 to 12. Cragin
states that the Kansas and the Denison specimens show "no differences of
specific value," but further information of a deciding nature is not forth-
coming.
Cragin's description of the species, Corbula crassicostata, is as follows:1
Cragin, Colo. Coll. Stud., 5, 1895, p. 61.
130 University of Texas Bulletin
"Corbula crassicostata, sp. nov.
"Shell triangular-ovate, gibbous ; nearly as broad as high, shorts ; gaping
posteriorly by a short, conically inflated, gently truncated rostrum, which
is placed high above the base of the shell ; unbones placed in advance of
the middle, that of the right valve only moderately high arched, its sum-
mit obtuse ; surface ornamented with very coarse, flattish-topped, concen-
tric ribs, separated by abrupt, deep narrow intervals. There are seven
or eight of the ribs on the basal half of a right valve the same number
of millimeters high.
"Measurements : Height 7.5, length 10, breadth about 7 mm.
"Occurrence: In arenaceous limestone bands of the Kiowa shales at
Belvidere, Kansas ; in Nos. 2-4 of the writer's 'Belvidere Section.'
"So far as the writer can judge from material now in hand, the similar
Corbula that abounds in the condition of casts and molds in Texas, presents
no differences of specific value from the Kansas shell above described. The
casts show that the pallial line is very sharply impressed."
CORBULA BASINIFORMIS n. sp.
PI. 9, figs. 7-24; PI. 10, figs. 7-9
MEASUREMENTS : Type-
Length 17.4 mm.
Height 12.1 mm.
Breadth 7.7 mm.
Difference in length of valves 2.4 mm.
HORIZON : Blue shale and clay-ironstone layers of upper half of Weno
formation, Red River region, abundant; Pawpaw clay, occasional.
LOCALITIES: 604, cut of Frisco track, three-fourths mile north of
Union station, Denison, Texas (type locality) ; 601, pit of brickyards one
and three-fourths miles southeast of Gainesville, Texas; numerous other
localities in Cooke and Grayson counties, Texas. Rare, as limonite stained
casts in the Fort Worth region.
DESCRIPTION : Shell small, inequivalve, almost smooth, with a short
pointed rostrum.
Right valve, exterior: Valve rather inflated, evenly rounded, its out-
line almost a truncated ellipse. As seen from directly above, the umbonal
angle is about 120 degrees ; the dorso-anterior margin is thereafter almost
straight for about one-third the greatest length of shell ; the anterior mar-
gin then describes an evenly rounded curve, a portion of an ellipse, which
continues to the middle of the ventral margin ; here the margin is more
nearly straight, but again curves more sharply dorsally and posteriorly,
and reaches the posterior (rostral) angle. This angle is 90 degrees and
is very slightly rounded-acuminate. The postero-dorsal margin is almost
Weno and Pawpaw Formations 181
straight, having a roughened, striate protruding area — the rostrum — reach-
ing to the umbo; and anterior to it is the straight posterior margin of
the valve.
The greatest height of the valve is near its center. Its convexity is
greater on the umbonal margin than on the ventral margin; from the
center the surface slopes gently to a line, marked in places by a prominent
growth line, below which the surface is curved at a sharply rounded angle
of 90 degrees to the margins of the valve, giving to the valve a charac-
teristic geniculated and basin-like appearance. The rim of the valve
thus slopes inward at all points except on the dorsal margin of the ros-
trum, so that the margin of the valve has a smaller circumference than
the prominent growth line mentioned above.
The ornamentation consists of radial striae and concentric growth lines.
The radial striae are fine, unbranched, wavy, or punctate lines which end
near the geniculation. The concentric growth lines are more conspicuous
(toward the ventral margin they resemble fine ribs), and pass posteriorly,
turning sharply dorsally at the line of junction of the main body of the
valve and the slightly developed rostrum. They then pass dorsally in
straight lines which give to the elongate triangular rostrum a roughened
striated appearance.
Right valve, interior: As viewed directly from above the interior of
the right valve has three prominent contours : the outer one is the margin
of the valve ; the middle one is a narrow groove, the junction between the
thicker outer (prismatic) shell layer and the thinner inner (porcellanous)
shell layer; the innermost contour is the limit of the main body cavity.
The first two are the shape of a long ellipse, and are situated a short
distance apart ; they begin at the antero-dorsal one-third of the prominent
tooth, and run concentrically around the anterior and ventral margins of
the valve, making an evenly rounded elliptical curve to the postero-ventral
extremity of the rostrum. The innermost contour encloses roughly a sub-
quadrate area whose boundary begins at the ventral margin of the tooth
and describes a slight curve to the dorsal end of the anterior adductor
scar. Here it runs almost straight ventrally with a slight posteriorward
convexity formed by the scar, in such a manner that a sharp-edged, cres-
cent shaped shelf, elevated above the main body cavity, is formed between
it and the middle contour mentioned. The scar is pear-shaped and its
inflated ventral end lies at the widest point of the shelf. The shelf con-
tinues along the interior of the ventral side of the visceral space to a point
one-third the way from the anterior end, and then fuses with the wall of
the valve. Just anterior to it lies the pallial line, a narrow groove with
a slight and irregular interior elevated crest which descends to the bottom
132 University of Texas Bulletin
of the visceral space and proceeds backward to a point underneath the
posterior adductor muscle scar. Here it turns backward making a 45
degree angle, then turns straight dorsally, making with its former course
a 90 degree angle, and reaches the lower angle of the scar. This rounded
triangular scar likewise lies on an elevation formed by the inner contour
mentioned, which passes dorsally and anteriorly, then turns anteriorly
reaching the ventral border of the tooth. It thus leaves dorsal to it and
posterior to the tooth, a kidney-shaped pit, into whose posterior border a
small tooth projects.
Left valve, exterior: This valve is smaller and distinctly shorter than
the right valve, but has almost the same depth. Its smaller length is due
to the shortness of the rostrum which fails to cover about one-half the
rostral area of the right valve, and thus leave a narrow wedge-shaped gap
for the siphon tubes. The left valve is in contour an obliquely truncated
ellipse. Seen from above, it has an umbonal angle of about 100 degrees
and an almost straight antero-dorsal margin. This continues as a sharply
and evenly rounded curve into the ventral margin which is gently curved,
but which posteriorly curves more sharply, reaching the tip of the ros-
trum. The postero-dorsal margin is roughly a straight line, except for a
slight bulging near the posterior half. The valve has a marginal gen-
iculation of about two-thirds the height of the corresponding one on the
right valve, and consequently a basin-like form for the entire valve.
The ornamentations consist of growth lines and weak concentric ribs,
of which there are about seven below the geniculation, and 26 or more
above it, the ribs decreasing in size in the dorsal one-third of the shell.
The ventral one-half of the valve, above the geniculation, bears about
12 ribs.
Left valve, interior: This valve has a truncate elliptical margin. It
may be divided into two regions : the visceral cavity and the rostrum. The
anterior part lacks the prominent shelf seen in the other valve. The
visceral cavity is a subquadrate depressed area from which a shallow
curved recess extends under the beak. Its margin is separated from the
posterior margin of the valve by the triangular shaped rostrum whose
inner surface is practically plane ; the dorsal and narrow two-thirds of the
triangle is occupied by the elliptical scar of the posterior adductor muscle ;
the anterior edge of this scar is smooth and forms the rim of the "shelf" ;
from it a perpendicular wall descends to the floor of the visceral cavity.
The ventral and wider one-third of the rostrum is the space for the siphon
tubes, and is plane with the floor of the visceral space.
From the lower end of the posterior adductor scar the narrow ribbon-
like pallial line descends ventrally for a short distance, turns sharply pos-
Weno and Pawpaw Formations 133
teriorly and then makes an acute re-entrant angle (25 degrees) passing
now anteriorly and almost perpendicularly to its former course; it runs
in almost a straight line to the anterior one-third of the valve, where it
gently curves upward meeting the postero-ventral corner of the scar of
the anterior adductor muscle.
This scar is roughly pear-shaped and its tip is continuous postero-dor-
sally with an elevated ridge which passes along the bottom of the pit for
the resilium. Dorsal to it, the elevated margin of the valve runs poster-
iorly, stopping short at the middle of this pit. This pit is subcircular and
lies anterior to the central tooth just dorsal to its mid-dorsal point is the
umbo. Posterior to it is a circular elevation which is separated by a con-
stricted neck from the post-adductor muscle scar.
LOCALITY : Cut in Frisco railroad, three-fourths mile north of Union
Station, Denison, Texas, in Weno marl, 20 feet below Quarry limestone
(locality 604).
CORBULA LITTORAL1S n. sp.
PI. 10, fig. 5
MEASUREMENTS: (Type) length of valve 18.0mm.
Length of rostrum 4.0 mm.
Height of valve _ 11.5 mm(?)
HORIZON: "Buff marl," near middle of the Weno formation, and
immediately below zone of abundance of Gervilliopsis invaginata (White)
in association with Venericardia wenoensis, Trochus laticonicits, cidarid
spines, Trigonia clavigera and Placosmilia sp.
LOCALITY : 601, pit of brickyard, one and three-fourths miles south-
east of Gainesville, Texas (type locality).
A fragmentary right valve, lacking umbo, antero-dorsal margin and
posterior half of ventral margin is apparently different from any other de-
scribed species, and it is considered best to describe it here. The indi-
vidual is rather similar to C. wenoensis Adkins.
Right .valve, exterior: The (restored) contour is elongate-triangular,
with probably a nearly straight antero-dorsal margin, a sharply rounded
anterior angle (probably about 60 degrees), a long nearly straight ven-
tral side, curving up only slightly to meet the ventral margin of the ros-
trum. The rostrum is short, truncate, and the form of an isosceles tri-
angle ; its rounded postero-ventral angle is 100 degrees ; its sharp postero-
dorsal angle is 110 degrees; an almost obsolete shallow oblique groove
separates it from the body of the valve, forming the base of the isosceles
triangle. The postero-dorsal side is nearly straight except for a slight
134 University of Texas Bulletin
convexity in its posterior one-third. The valve is distinctly rotund and
elevated.
The ornamentation consists of 12 coarse rounded concentric ribs, and
a number of fine growth lines in the umbonal region; the. ventral half of
the height contains nine of the coarse ribs. These ribs turn dorsally along
the anterior end of the rostrum and just posterior to the oblique shallow
groove, making an angle of 95 degrees to 100 degrees. The ribs near
this angle bear each about four or five fine growth lines. The edges of the
ribs appear as thin slightly imbricated and overlapping lamellae. Dorsal
to the angle, the rostrum is conically inflated, the width of the fold in-
creasing postero-ventrally and at the posterior end occupying the whole
height of the rostrum. Dorsal to the inflation is a narrow concurrent
and slightly divergent depression. The rostrum is half the height of the
shell and is very close to the ventral margin. The ribs are unbranched and
continuous from the anterior to the posterior ends of the valve. They are
elevated with rather sharply rounded tops and are separated by plane
bottomed, vertical-sided valleys whose width is one-sixth that of a rib.
Remarks: The following species of Corbula are to be found in the
literature on the Comanchean : C. pikensis Hill (Trinity division) ; and
C. crassicostata Cragin, Kiowa, Kansas, and (by implication) in the
"ochreous shell-conglomerate of the Denison beds, Denison, Texas."
C. basiniformis is distinguishable from the other species mentioned by its
relatively unornamented surface and its geniculate margin. C. littoralis
is distinguished from the others by its few coarse elevated and broad ribs ;
C. wenoensis is distinguished from C. littoralis by its smaller size, its
different and less elongate form, its greater number of ribs, the more dor-
sal position of its rostrum, the shape and relative height and position of
the rostrum, and by the internal characters as described.
CYPRIMERIA WASHITAENSIS n. *p.
PI. 9, figs. 1-6
Type
MEASUREMENTS: PL 9, fig. 1 PL 9, fig. 4 PL 9,.fig. 2
Height 52.0 52.0 76
Length 58.5 59.0 77+
Breadth 15.0 17.5 25
HORIZON: Weno formation, upper and middle thirds, shale facies.
LOCALITIES : 604, cut of St. Louis and San Francisco Railway, one
mile north of the Union Station, Denison, Texas (type locality) ; 601, pit
of brickyards, three-fourths mile southeast of Gainesville, Texas.
Weno and Pawpaw Formations 135
DESCRIPTION: Shell subovate, inequilateral, subequivalve, beaks
pointed anteriorly (prosogyrate) ; surfaces of both valves covered with
numerous, simple, fine, striaeiform, concentric growth lines, and having a
few widely spaced, coarser growth rings. Shell preserved, interior filled
with ironstone. The beaks are inconspicuous, recurved anteriorly forming
anterior to them a small notch in the margin and are rounded, incurved
and approximate ; anterior to them the margins of the valves are in contact
and the growth lines are imbricated and separated, making several lines
parallel to the margins of the valves. Posterior to the beaks is a much
wider triangular depression between the margins of the valve. It runs
from the umbo backwards to the postero-dorsal, angle; its bottom is the
apposed inner dorsal margins of the valves, its top the separated outer
dorsal margins, while its sides consist of growth lamellae terminating
abruptly and together constituting the thickness of the valves at this
point. The groove in one individual contains over the medial half of its
length a well preserved external hinge ligament. This has a chitinous
appearance but is replaced by calcareous material.
The dentition is approximately that of Cyprimeria Conrad. The hinge
of the left valve consists of two posterior lamellae, two teeth and an an-
terior lamella. The most dorsal posterior lamella is very broad and ob-
lique, and is nearly parallel to the inner dorsal shell margin, which it has
overgrown. It is roughly lanceolate or blade-shaped, the point being di-
rected toward the umbo, the curved back directed ventrally, the edge di-
rected dorsally and a narrowed portion directed postero-dorsally. It is
separated by a narrow groove from the shorter second posterior lamella,
which lies parallel to it and is coalescent with its umbonal half. Ventral
to this lamella there is a narrow, deep, elongated pit, which separates it
from the more posterior tooth. This pit in one individual contains a mass
of brownish material chitinous in appearance but in fact calcareous. The
two teeth are sharp, ridge-like and elongated, making an angle of about
60 degrees with each other; they are remote and are separated by a tri-
angular area, raised centrally. Running anteriorly from the base of the
tooth is an elongate elevated margin which may be taken as an anterior
lamella. Dorsal and parallel to this is an elongate groove which is bounded
dorsally by the upturned inner dorsal edge of the valve. Parallel and an-
terior to the anterior tooth is a narrow deeper depression the length of the
tooth, which anteriorly connects with the groove. Below the teeth is an
elongated area of small pits and punctations on the dorsal portion of the
inner surface of each valve. Cyprimeria crassa Meek has been recorded1
'Hill, Annotated Check List, p. 14.
136 University of Texas Bulletin
from the Eagleford shales near Denison, Texas and Cragin considers it to
be widespread in the Fredericksburg division in South Texas. This species
is stated to differ from C. texana (Roemer) in its large thickness and size.
Cragin1 also records Cyprimeria sp. aff. excavata Morton from the Eagle-
ford shales ("top of Ostrea quadriplicata beds"). Still a larger Cypri-
meria, called C. gigantea* by Cragin is recorded from the Grayson marl
near Roanoke, Texas ; we have found similar individuals in the Grayson
at Roanoke, Denison, Burleson and elsewhere. Our species appears to be
close to Cyprimeria texana (Roemer) which is known as casts from the
Fredericksburg division. One individual of this species at hand shows a
simple entire pallial line, some details of dentition, and papillae represeting
the pits on the inner surface of the valves below the hinge, as mentioned
above in the description of C. washitaensis and as figured by Roemer and
Conrad for C. texana. The two species seem to differ but slightly, yet in
view of the uncertain systematic position of the Fredericksburg species
and its poor preservation it is thought best to describe the present material
separately. The relations of the pallial line to the posterior adductor
muscle scar are entirely different in the two species and the scar is of a
different shape. In a fragment of the left valve of a large individual of
C. washitaensis from near Denison the scar is subquadrate in shape and
the pallial line attaches directly to its lower anterior corner, while in
Roemer's figure3 of the impression of the right valve, the scar is an inclined
oval and its postero- ventral end lies in a prominent loop in the pallial line ;
this loop is missing in our species. Roemer's species also appears to have
a considerably sharper marginal curvature just anterior to the umbo than
has C. washitaensis, of which however I have not yet found any interior
casts for direct comparison, all of the known material consisting of nac-
reous shells.
REMONDIA ? ACUMINATA (Cragin)
PL 6, fig. 1
This species does not have close similarities in form to that figured
by Gabb," yet the hinge is rather similar. Stanton5 has figured and dis-
cussed the species of this genus. The hinge is here figured (PI. 6. fig. 1).
The species has an acuminate tip, nearly straight antero-dorsal and postero-
dorsal margins and a gently rounded ventral margin. Posteriorly the
'Cragin, Geol. Surv. Texas, 4th Ann. Report., pp. 176-7, 1893.
2Cragin, Ibid., p. 176.
sRoemer, Kr. Texas, pi. VI, fig. 8a.
*Gabb, Geol. Surv. Calif., Pal. II, p. 270, pi. 36, figs. 17-17a, 1869 (Remondia furcata).
5Stanton, Proc. U. S. N. M., XIX, 299-301, 1920.
Weno and Pawpaw Formations 137
shell is incurved to form a rostrum-like constriction. There are 8 to 15
roughly concentric, sharply elevated ridges which contract towards the
posterior end of the shell.
The species is occasional in the lower Weno marl of the Fort Worth
region, especially at locality 618, in association with Pecten georgetown-
ensis, Ancycloceras bendirei. Schloenbachia wintoni, Turritella worthensis,
and Venericardia wenoensis.
GASTROPODA
AMBERLEYA GRAYSONENSIS n. sp.
PI. 6, fig. 5
MEASUREMENTS : ( Type individual ) .
Height 21.0 mm.
Breadth (estimated) 17.2 mm.
Last whorl, height 11.0 mm*.
Last whorl, breadth 10.0 mm.
HORIZON: Basal stratum of Weno shale, in association with Ostrea
quadriplicata, Gryphea washitaensis, Salenia sp. and various echinoids.
LOCALITY: 606, just south of Frisco track, two and one-half miles
north of Denison, Texas.
DESCRIPTION : Shell conical, turreted, spiral angle about 63 degrees
(estimated, shell of type distorted) ; volutions three or more, the terminal
one being over one and one-half times the diameter of the next smaller one.
Volutions angular, projecting, cross-section somewhat pentagonal. The
volutions bear externally three coarse revolving ridges, of which the outer
ones form the upper and lower shoulders of the volution. These ridges
are equal and equally spaced, the distance between them being about two
times the width of a ridge. The volution is crossed transversely by lan-
ellar growth lines with thin overlapping irregular edges. From the center
of the spire these trend sharply forwards, and crossing the first heavy ridge
then pass obliquely across the outer face of the volution and after travers-
ing the marginal strip of the volution on the other side of the ridges, dis-
appear at the suture. They form slightly elevated imbricated low nodes
on crossing the three spirals. Umbilicus absent, aperture indeterminate.
138 University of Texas Bulletin
TROCHUS LATICONICUS n. sp.
•
PI. 10, figs. 30-31
MEASUREMENTS : I II
Height 9.0 7.8
Greatest width 8.9 8.8
Aperture, height 3.0 2.5
Aperture, width 4.4 4.0
HORIZON: Weno formation, shale facies. Has so far been found
only in the zone of Gervilliopsis invaginata (White) .
TYPE LOCALITY: 601, pit of brickyard, one and three-fourths miles
southeast of Gainesville, Texas.
DESCRIPTION: Shell small, conical, angulated. Volutions five of
which, two earliest in this type, are nearly smooth. Form trochoid, apical
angle 55 degrees, sutures impressed, ornamentation consists of a coarse,
revolving spiral on the keel, ten finer spirals above, the alternate ones
being coarser and consisting of equal low rounded tubercles, the others
being straight fine revolving elevated ridges ; and below the keel ten eqaul
similar non-tuberculate spiral ridges, each about half the width of the
intervening valley. Growth lines numerous, fine, sigmoid, oblique to the
ridges. Umbilicus concealed, small if any; aperture broken; probably
obliquely oval. The next tuberculate ridge above the keel is thicker than
the others and the keel and it lie just above the suture on the younger
whorls and form a distinct angulation at the base of each volution. The
shell on the last volution is thick (one half mm.) and the external markings
well preserved.
Trochus sp. Shattuck1 from the Buda limestone at Austin differs from
our species in having a larger apical angle (66 degrees) and straighter,
non-angulated sides. Trochus texamts Roemer2 from the Barton Creek
(Austin, Texas) fauna of the Edwards limestone differs locally from our
species in the nature of the ornamentation, the straightness of the sides
and apparently in the shape of the aperture. This species is also described
as having a pointed tooth on the inner margin of the outer lip.
iShattuck, U. S. G. S. Bull. 205, p. 31, pi. XIX, figs. 2-3.
2Roemer, Pal. Abh., vol. 4, pt. 4, p. 15, pi. 1, fig. 13.
Weno ami Pawpaw Formations 139
HELICOCRYTPUS MEXICANUS Bose
1910: Helicocryptus mexicanus Bose, Inst. Geol. Hex., Bol. 25, p. 140, pi. 46, figs. 1-6;
pi. 47, fig. 1.
A single individual lacking the mouth but otherwise well preserved and
agreeing with the original description, was determined by Dr. Bose as be-
longing to this species.
LOCALITY : 714, near Fort Worth, Texas, in the basal Pawpaw clay.
NERITA .p.
PI. 10, fig. 28
This fossil is found in the "buff marl" of the Weno brickyards at Gaines-
ville, Texas, in association with Trochus laticonicus, Venericardia weno-
ensis, and other fossils listed in the geological section of this locality.
NERITINA .p.
PI. 10, fig. 27
This small calcitic fossil is one of a group of peculiar small fossils as-
sociated in the "buff marl" of the brickyard pit, near Gainesville, Texas.
The others are Trochus laticonicus Adkins, Nerita sp., Venericardia weno-
ensis Adkins, Placosmilia spp., Trigonia clavigera Cragin, Leioddaris
spines, Corbula littoralis Adkins, Pecten sp. and numerous widely distrib-
uted Weno fossils.
•
ANCHURA MUDGEANA White
PI. 10, figs. 39-40
1879: Anchura mudgeana White, llth Ann. Kept. Geol. and Geogr. Surv. Terr., p. 312,
pi. 7, fig. 3a-b.
1889: Anchura (Drepanocheilus) mudgeana Hill, Geol. Surv. Texas Bull. 4, p. 19.
1894: Anchura mudgeana Hill, Bull. Geol. Soc. Amer., vol. 5, p. .
1918: Anchura mudgeana Stephenson, U. S. G. S. Prof. Paper 120-H, p. 141.
This common species of the Weno shale at Denison and Gainesville has
not been found outside the Red River region, to my knowledge. It is con-
spicuous in the ironstone and blue shale layers of the Weno in association
with a large nacreous fauna including Corbula spp., Nucula spp., Turritella
sp., Cerithium sp., Natica sp., and others. It differs from Anchura pro-
labiata White in having a single instead of a double lip ; and from A. ruida
140 University of Texas Bulletin
White and A. haydeni White1 in having a rounded, tabulated, externally
directed lip instead of an upturned sharply pointed one. It differs from
Anchura monilifera Gabb2 found at Arivechi, Sonora, in the less elongate
form and greater apical angle, in the greater width of the aperture, and
in the tabulated lip.
NATICA *p.
PI. 10, fig. 29
A small nacreous Natica is known from the ironstone layers of the Upper
Weno shale of the Red River region. It is preserved with the slightly
altered calcareous shell. Locality 601, pit of brickyards near Gainesville,
Texas.
LUNATIA »p.
PI. 10, fig. 38
This Weno species has a nacreous preservation and occurs in both the
Upper Weno shale and the interspersed clay-ironstone seams. It is oc-
cosional in the ironstone heap thrown out of the brickyards pit near Gaines-
ville, Texas.
GLOBICONCHA *p.
PI. 10, fig. 41
This large species is rare in the Red River region, and is known from
the clay-ironstone layers of the upper part of the Weno shale, in associa-
tion with Protocardia sp. aff. multristriata (Shumard), Turritella gray-
sonensis, Cinulia washitaensis, Gervilliopsis invaginata, Schloenbachia win-
toni, Cambarus ? sp. and other Upper Weno fossils. Locality, 601, near
Gainesville, Texas.
TURRITELLA GRAYSONENSIS n. sp.
PI. 10, fig. 43
MEASUREMENTS :
Type, greatest height ----------------------- 36.0 mm.
Width of last volution _______________________ 11.5 mm.
Section of last volution, height _______________ 7.5 mm.
Section of last volution, width ________________ 7.0 mm.
e, llth Ann. Kept., U. S. G. and G. S. Terr., 1879.
"Gabb, Geol. Surv. Cal., Pal. II, p. 262, pi. 35, fig. 7, 1869.
Weno and Pawpaw Formations 141
HORIZON: Weno shale and ironstone, abundant; Pawpaw clay and
sand, rare. Rare south of the Red River region.
LOCALITY : This is the common nacreous Turritella of the Weno iron-
stone and clay at Denison, Gainesville, and elsewhere in the Red River
region. Locality 604, Frisco cut three-fourths mile north of Union Sta-
tion, Denison, Texas (type locality) ; 601, near Gainesville, Texas.
DESCRIPTION: Shell turreted, steep, spiral angle 17 degrees; ten
or more volutions, straight-sided, sutures sharply impressed, angles of
volutions sharply rounded, surface almost smooth, bearing about fourteen
lightly tuberculate spiral lines of unequal height. Of these, ten lie on
the side of the volution and four below the shoulder. On the terminal
volution of the type these are arranged as follows :
Beginning at the suture, the first ridge is strongest and bears widely
spaced low obscure tubercles with flat spaces between; the thickness of
this rib equals the width of the space separating it from the second rib.
The second, fifth and seventh ribs are slightly narrower, but are ribbon-
like and low in proportion to their breadth and have slight nodular eleva-
tions widely spaced from each other. The other ribs are low, subequal and
have rounded tops and slight nodular elevations at wide intervals. The
last four ribs lying beyond the shoulder of the volution are relatively nar-
rower and more elevated than those on the flanks, and the inner three are
closely spaced, being separated by about the width of a rib ; the last rib
is more widely separated but is the same size. The rest of the volution
next to the umbilicus is smooth except for one or two obsolete spiral ribs.
In the intervals between the ribs mentioned there are three to five fine
equal raised lines. The transverse growth lines are prominent and sig-
moid, and resemble those in T. bravoensis Bdse, but are finer. Aperture
unknown ; crass-section of volution sub-quadrate, outer side straight, inner
side rounded.
This species is separated from Turritella bravoensis Bdse, T. budaensis
Shattuck, and T. planilateras Conrad by having the tubercles very low,
and depressed, instead of coarse and prominent. It is separated from
T. leonensis Conrad, T. marnochi White, and T. denisonensis Cragin in
having a greater number of spiral ridges and more tubercles in each ridge.
Cragin1 describes without figuring, a variety under the name of T. kan-
sensis, which has less crowded revolving ridges than our species. Like-
wise, T. seriatim-granulata Roemer2 differs from T. wenoensis in having
only five elevated tuberculated ridges, the middle one of which is flanked
iCragin, Notes on some fossils of the Comanche series, Science, n. s., vol. 6, pp. 134-
136, 1897.
zRoemer, Kr. Texas, p. 39, pi. 4, fig. 12.
142 University of Texas Bulletin
on each side by a low, non-tuberculate ridge. The ridges are wider and
more prominent than in our species and the intervening spaces much nar-
rower ; the tubercles are more widely spaced ; the fine secondary revolving
lines are apparently lacking; and the contour is more angular. Roemer's
species is also figured as having a smaller apical angle (about 12 degrees).
TURRITELLA WORTHENSIS n. sp.
PI. 10, fig. 42
MEASUREMENTS: Type length of fragment 26 mm.; width (esti-
mated) 14.5 mm.
HORIZON: Basal Weno formation, marl facies. Abundant in the
Fort Worth region in association with Ancycloceras bendirei, Remondia
acuminata and Pecten georgetownensis.
LOCALITIES: 618, near Fort Worth, Texas (type locality); exten-
sively distributed in Tarrant County, Texas.
DESCRIPTION: Shell conical, steeply turreted, apical angle 23 de-
grees, with six or more volutions. Shell nearly straight sided, sutures
impressed, surface with usually six nearly elevated spiral ridges bearing
conspicuous, equal, equally-spaced, rounded tubercles. Beneath this are
two parallel thin spiral ridges with obsolete tubercles. These form the
bottom of the volution, and the uppermost of the six ridges mentioned,
which is longer than the others, forms the top. Between each two ridges
are four to six fine non-tuberculate spiral lines, but exceptionally one or
two of these may be thickened, giving the appearance of an alternating
series of fine and coarse revolving ridges on the volution. In most of the
material at hand the six revolving ridges are equally spaced, and are sep-
arated by a depression only slightly wider than one of the ridges. The
tubercles are equally spaced on all the ridges, and number about 65 on
the last volution. These tubercles decrease in size on the earlier volutions,
and all are present in the youngest stage examined.
Transverse growth lines are not visible. The details of the aperture
are not preserved. The cross-section is rounded and triangular, the ex-
ternal side of the volution being longest. Below the shoulder of the usually
tuberculate volution are about four impressed lines, of which the two al-
ready mentioned are not covered by the succeeding volution. Below this
point the volution is smooth.
Many species of Turritella have been described from the Texas Coman-
chean, and some of these are indeterminate, on account oi faulty figures
and description, or lack of necessary information concerning stratigraphy
and locality.
Weno and Pawpaiv Formations 143
The present species is nearly straight-sided and is slightly angulated,
while in T. bravoensis Bose1 the middle rows of tubercles form a conspicu-
ous angular projection on each volution. The number of rows of tubercles
is greater than in Bb'se's species and the tubercles are more crowded in
the rows. The conspicuous transverse striated growth lines of his species
are absent in our material. T. pkmilateras Conrad2 is somewhat similar
in form to our species, but has a prominent alternation of tuberculate and
smooth spiral ridges, while in our species the intermediate lines are tuber-
culate and do not approach the main ridges in thickness. T. budaensis
Shattuck3 has the rows of tubercles diverse, the second row from the suture
being most prominent, and the form is more angulated than in our species.
T. worthensis is at once separated by its strong tubercles from the faintly
tuberculate or granulated species, T. seriatim-granulata Roemer4 (Freder-
icksburg, Lower Washita), T. marnochi White,5 T. leonensis Conrad (Fred-
ericksburg)6 and T. denisonensis Cragin7 (Mainstreet, Grayson).
Ellisor8 has described several species of TurriteUa of which only T. man-
chacensis (Buda) and T. washitensis (Buda> seem to approach the present
species in ornamentation or form.
CINULIA WASHITAENSIS n. .p.
PL 10, figs. 33-37
1920: Cinulia sp. Winton and Adkins, Univ. Texas Bull. 1931, p. 66.
MEASUREMENTS :
Total height 15 mm.
Total breadth . 14 mm.
Body whorl, excluding lip, height 10 mm.
Body whorl, excluding lip, breadth 10 mm.
Breadth of lip 4 mm.
HORIZON: Weno blue shale and clay-ironstone layers, middle and
upper portions of the formation, especially in the Red River region.
LOCALITY : 601, pit of brickyards, one and three-fourths miles south-
ifiose, Inst. Geol. Mex., Bol. 25, p. 149, pi. 31, figs. 8-9; pi. 32, figs. 1-2, 1910.
'Conrad, Mex. Bdry. Surv., Vol. 1, Pt. II, p. 158, pi. 14, figs, la-b, 1857.
"Shattuck, U. S. G. S. Bull. 205, p. 31, pi. XIX, figs. 4-6, 1902.
4Roemer, Kr. Texas, p. 39, pi. 4, figs. 12a-b, 1852.
'White, U. S. G. and G. S. Terr., llth Ann. Kept., pp. 314-315, pi. 7, figs. 5a-b, 1879.
«Conrad, Mex. Bdry. Surv., Vol. 1, Pt. II, p. 165, pi. 21, figs. 7a-b, 1857.
'Cragin, Colo. Coll. Stud., 5, p. 65, 1895.
"Ellisor, Univ. Texas Bull. 1840, 1920.
144 University of Texas Bulletin
east of Gainesville, Texas (type locality) ; 604, cut of St. Louis and San
Francisco Railway, three-fourths mile north of Union Station, Denison,
Texas. Occasional in Cooke and Grayson counties, Texas. About 25 in-
dividuals found.
DESCRIPTION : Shell of medium size, sub-globose, total outline sub-
elliptical; four volutions, of which the last is much the largest and occu-
pies two-thirds the height of the shell. Surface ornamented with evenly
rounded equal revolving lines, about 25 on the last volution. Between
the lines are concave depressions each about one and one-half times the
width of a line. These contain numerous equally spaced vertical cross
striations, which run perpendicular to the depressions and to the adja-
cent revolving lines. Aperture elongate, rounded-cuneate, narrowed at
the top and enlarged at the bottom. Outer lip much thickened and rounded,
elongate, extending the length of the two last volutions in the type (slightly
shorter in other individuals), and bearing on the inner margin about 14
nearly equal blunt tubercles in two equal groups. The inner lip is flat
and expanded and bears on its apertural margin three elevated spiral folds
or laminae which project into the aperture ; these are thickened and rounded
at their free margins ; the basal two lie almost horizontal while the upper
one is directed somewhat downwards and is concealed underneath the
jnner lip. Viewed from outside the outer lip is very broad and thick-
ened and bears about seven irregular coarse overlapping laminae.
This species resembles Cinulia tarrantensis Cragin1 of the Goodland
limestone near Fort Worth, but differs in several respects. C. tarrantensis
is poorly described and figured and some of its critical points are inde-
terminate, no further material having been discovered from the type
locality, Goodland limestone near Benbrook, Tarrant County, Texas. The
type apparently is lost, or at least it is not in the other Bumble Survey
material at Austin. Cinulia is extremely rare in the Goodland limestone
of the Fort Worth region. The species appears to differ from C. wash-
itaensis in having a narrow and much less imbricate lip and in having
the spire lower in proportion to the length of the lip. In Cragin's species
the lip does hot seem to reach the top of the body whorl, while in the type
of our species it is more elongate, extending the whole length of the term-
inal and next adjacent whorls instead of only three-fourths of the term-
inal whorl. In some other individuals it is lower, but never so low as in
C. tarrantensis. The figure of C. tarrantensis shows the angulation of
the turns above the body whorl to be pronounced, while in our species
also differs in numerous details. The outer lip is broader in proportion
Cragin, Geol. Surv. Texas, 4th Ann. Kept., p. 223, pi. XLII, fig. 1.
Weno and Pawpaw Formations 145
these turns are rounded. The shape of the aperture and of the teeth
to the body and bears much coarser imbricated lamellae than in Cragin's
species; the aperture is more slender throughout and is noticeably more
compressed below; the sub-central crenulate region of the inner edge of
the outer lip is distinctly angular ; the inner lip is broader and the three
teeth placed differently, the two terminal ones being more closely spaced.
Our species is apparently larger than C. tarrantensis, and comes from a
higher horizon.
The unfigured and indeterminate species Cinula ? texana (Shumard)2
was described from the Fredericksburg division of Bosque County; its
description will apply to most species of the genus. C. rectilabrum Gabb1
is a lower species and bears on its inner lip two teeth instead of three;
it is more slender, more pointed apically, and has narrower lips and a
more elongate aperture. Cinulia pelletti Whitney and C. conradi Whit-
ney,3 both. from the Buda limestone differ in several respects from the
Weno species, the former in the proportions of the shell, the height and
shape of the aperture, and the thickness of the outer lip, the latter in the
shape, size and number of costellae.
PROTOZOA
NODOSARIA TEXANA Conrad
PI. 11, fig. 2
This characteristic foraminiferean shell has already been described*
in some detail and the features mentioned apply to the Weno and Pawpaw
material at hand. The fossil ranges in North Texas through the upper
third of the Weno limestone and the base of the Pawpaw clay. The in-
dividuals are generally scattered, but also rarely occur in slabs. At Fort
Worth there is a zone of abundance at a point about 18 feet below the top
of the Weno formation, which is found at this stratigraphic level every-
where between the Red River and the Brazos. This zone appears to be
different from the common Del Rio Nodosaria zone of West Texas, for
prevailingly in West Texas the zone of abundance of Nodosaria is in the
top of the Del Rio clay .iust underneath the Buda limestone, and the fossil
is scattering in the middle Del Rio clay. Near Del Rio, Texas, where the
formation is about 200 feet thick the Nodosaria slabs are prominent near
the top, and near the Chisos Mining Company, Brewster County, where
iGabb, Geol. Surv. Calif., Pal. II., p. 264, pi. 35, figs. 10-10a.
'Shumard, Trans. Acad. Sci., St. Louis, I, 1860, 597.
"Whitney, Trans. Texas Acad. Sci., XII, p. 23, pi. 10, figs. 9-11.
«B6se, Inst. Geol. Mex., Bol. 25, p. 177, 1910; Adkins and Winton, Univ. Texas Bull.
1945, p. 76, 1920.
146 University of Texas Bulletin
the Del Rio clay is 120 feet or more thick, the zone of abundance of
Nodosaria is above the occurrence of Exogyra cartledgei Bose, which lies
10-30 feet below the Buda limestone.1 This level probably corresponds
to the Grayson formation of North Texas. Nodosaria is rare at Austin
in the middle Del Rio clay. At Cerro de Muleros, which is in the northern
facies, it is reported as occurring in subdivision 5 (Duck Creek and Fort
Worth), and as abundant in subdivision 6 (Denton, Weno and Pawpaw) ;
this is its lowest recorded occurrence.3
BIBLIOGRAPHY
Adkins, W. S., and Winton, W. M.: Paleontological Correlation of the Fredericksburg
and Washita Formations in North Texas. Univ. Texas Bull. 1945, 1920. (Bib-
liography.)
Berry, E. W. : The lower Cretaceous floras of the world. Maryland Geol. Surv., Lower
Cretaceous, pp. 99-151. Baltimore, 1911.
The upper Cretaceous floras of the world. Maryland Geol. Surv., Upper
Cretaceous, pp. 183-313. Baltimore, 1916.
Bose, Emil: Monografia geologica y paleontologica del Cerro de Muleros, etc. Inst.
Geol. Mex., Bol. 25, 1910.
On a new Exogyra from the Del Rio clay and some Observations on the
Evolution of Exogyra in the Texas Cretaceous. Univ. Texas Bull. 190?, 1919.
Cotteau, G.: Echinides, in Paleontologie francaise.
Cragin, F. W. : A contribution to the Invertebrate Paleontology of the Texas Creta-
ceous. Geol. Surv. Texas., 4th Ann. Rept., pp. 141-294.
Descriptions of Invertebrate fossils from the Comanche Series in Texas,
Kansas, and Indian Territory. Colo. Coll. Stud., 5, 1895, 49.
Dumble, E. T.: The Geology of East Texas. Univ. Texas Bull. 1869, 1920
Grossouvre, A.: Recherches sur la Craie Superieure. I. Stratigraphie generale.
II. Paleontologie. Paris, 1893-1901.
Haug, Emile: Traite de Geologic. Paris, 1911.
Hill, R. T.: The Geology of the Black and Grand Prairies of Texas. U. S. G. S. 21st
Ann. Rept., Pt. 7, 1901.
Geology of the Territory adjacent to the Red River in Arkansas, Texas.
and Indian Territory. Bull. Geol. Soc. Amer., 5, pp. 297-338, 1893.
Noetling, F.: Die Fauna der baltischen Cenoman-geschiebe. Pal. Abh., BH. II. heft 4,
1885.
Pervinquiere, L.: Etudes de paleontologie tunisienrie. I. Cephalopodes des terrains
secondaires. II. Lamellibranches et gastropodes des terrains secondaires. Paris,
1907.
Pervinquiere. L. : Sur quelques ammonites du cretace alger'en. Mem. Soc. Geol. France,
Paleontologie, tome xvii, fasc. 2-3, Mem. No. 42, pp. 1-86, pis. 1-7 (x-xvi), 1910.
'Bose, Univ. Texas Bull. 1902, p. 19, 1919.
-Bose, Inst. Geol. Mex., Bol. 25, pp. 24-26, 1910.
Weno and Pawpaw Eormations 147
Richardson, G. B.: Report of a reconnaissance in Trans-Pecos Texas north of the
Texas and Pacific Railway, Univ. Texas Mineral Surv., Bull. No. 9, 1904.
Sayn, G. : Les ammonites pyriteuses des marnes valangiennes du sud-est de France.
Mem. Soc. Geol. France, Paleontologie, tome 9, Mem. No. 23, pis. 1-6 (vi-x, pi. vii
repeated), pp. 1-66, 1901.
Sellards, E. H.: The Geology and Mineral Resources of Bexar County. Univ. Texas
Bull. 1932, 1920.
Sladen, P., and Spencer, W. K. : A monograph of the British fossil Echinodermata,
Asteroidea. Paleontogr. Soc.
Szajnocha, Ladislaus: Zur Kenntniss der mittelcretacishen Cephalopodea-fauna der
Inseln Elobi an der Westkiiste Afrika. Denkschr. d. Kais. Akad. Wiss., Wien.,
XLIX, pp. 1-8, pis. 1-4, 1884.
Whitney, F. L.: The Echinoidea of the Buda limestone. Bull. Amer. Pal., No. 26, 1916.
Winton, W. M., and Adkins, W. S.: The Geology of Tarrant County. Univ. Texas
Bull. 1931, 1920.
PLATE 1
Flickia, Schloenbachia, Mortoniceras, Acanthoceras
150 University of Texas Bulletin
PLATE l.
Flickia, Schloenbachia, Mortoniceras, Acanthoceras Plate 1
Figures 1-3. Flickia boe«ei n. sp Page 85
Rare, basal Pawpaw formation, marl-clay transitional area. Fig. 1, type indi-
vidual, side view, x 4.7; fig. 2, same individual, ventra' view, x 4.7; fig. 3,
same individual, x 1.33. Locality: 714, near Fort Worth, Texas.
Figure 4. Flickia (?) bosquensis n. sp Page 87
Rare, top of Exogtfra arietina horizon, middle Del Rio clay (equivalent of base
of the Grayson formation). Locality: cliff on west bank of the South Bosque
River, 100 yards south of the bridge of the Speegleville road, and 5.5 miles
west of the courthouse at Waco, Texas. Type individual, side view, x 2.0.
(See PI. 4, fig. 11.)
Figure 5. Schloenbachia sp
Rare, basal Pawpaw clay. Locality: 714, near Fort Worth, Texas.
Figures 6-10, 18-19, 26. Mortoniceras worthense n. sp Page 91
Abundant, Pawpaw formation, base, clay facies.
Fig. 19, type individual, x 4.0. Locality: 723, near Fort Worth, Texas; figs. 10,
26, same locality, x 4.0. Other figures, x 2.0, same locality.
Figures 11-13, 15-17, 20-25. Acanthoceras worthense n. sp Page 93
Abundant, Pawpaw formation, base, clay facies.
Fig. 12, type individual, x 2.0. Locality: 723, near Fort Worth, Texas. Other
individuals, x 2.0, same locality.
Figure 14. Schloenbachia wenoensis n. sp Page 89
Rare, Pawpaw formation, base, clay facies. Fig. 14, type individual, x 2.0.
Locality: 723, near Fort Worth, Texas.
University of Texas Bulletin No. 1856
PLATE 2
Scaphites, Hamulina, Metopaster, Comptonia
152 University of Texas Bulletin
PLATE 2.
Scaphitei, Baculites, Ptychoceras, Metopaster, Comptonia Plate 2
Figures 1-12. Scaphites hilli Adkins and Winton Page 79
Occasional, basal 10 feet of the Pawpaw formation, clay facies, sparse outside of
Tarrant County region. Fig. 1, type individual, x 4.0, ventral view, showing
suture and mid-ventral groove. Locality: 714, near Fort Worth, Texas. Fig.
2, individual showing venter with sutures outlined in the hematite and limo-
nite areas, x 4.0. Locality: 714. Fig. 3, individual showing suture, dorso-
lateral tubercle, and aperture, x 4.0. Locality: 714. Fig. 4, same individual,
reverse side, x 6.0. Figs. 5, 6, individuals x 4.0. Locality: 714. Fig. 7, indi-
vidual showing uncoiled portion and dorso-lateral tubercle, x 2.0. Locality:
723, near Fort Worth, Texas. Fig. 8, individual showing uncoiled portion,
tubercle and juvenile suture, x 4.0. Locality: 723. Figs. 9-12, showing rib
variations, x 4.0. Locality: 723.
Figures 13, 15-18. Scaphites sp. aff. hilli Adkins and Winton
Occasional, Pawpaw clay, base. Fig. 14, x 3.0; figs. 13, 16-18, x 2.0, showing rib
variations. Locality: 713, near Fort Worth, Texas.
•
Figure 14. Metopaster hortensae Adkins and Winton Page 97
Rare, Pawpaw formation, base, clay facies. Type individual, aboral side, x 2.0.
Locality: 714, near Fort Worth, Texas.
Figure 19. Comptonia wintoni n. sp Page 97
Rare, Pawpaw formation, base, clay facies. Type individual, aboral side, x 3.0.
Locality: 714, near Fort Worth, Texas.
Figures 20-22. Baculites comanchensis n. sp Page 74
Occasional, Pawpaw formation, base, clay facies. Type individual. Fig. 21, x 4.0.
Locality: 719, near Fort Worth, Texas. Fig. 20, x 2.0, same locality. Fig. 21,
x 2.0. Locality: 714, near Fort Worth, Texas,
Figures 23-26. Hamulina worthensis n. sp Page 71
Rare, basal Pawpaw clay. Type individual, Fig. 26, x 5.0, showing suture.
Locality: 714. Fig. 23, individual showing form of curve and short limb,
x 4.0. Locality: 714. Fig. 25, same individual, ventral view, x 2.0. Fig. 24,
individual showing form of long limb and of curve, x 4.0. Locality: 714.
Individuals of Figs. 23, 24 in museum of Texas Christian University, Fort Worth,
Texas.
University of Texas Bulletin No. 1856
Plate 2
PLATES
Turrilites, Acanthoceras, Schloenbachia
154
University of Texas Bulletin
PLATE 3.
Turrilites, Acanthoceras, Schloenbachia Plate 3
Figures 1, 6. Turrilites worthensis Adkins and Winton Page 78
Abundant, Pawpaw formation, base, clay facies. Fig. 1, x 4.0; locality: 714,
near Fort Worth, Texas. Fig. 6, showing portion of suture, x 4.0; locality:
714, near Fort Worth, Texas.
Figures 2, 4. Turrilites sp Page 78
Abundant, Pawpaw formation, base, clay facies. x 4.0; locality: 714, near Fort
Worth, Texas.
Figures 3. 7. Turrilites bosquensis n. sp Page 76
Rare, top of Exogyra arietina horizon, middle Del Rio clay (equivalent of base
of the Gray son formation). Locality: cliff on west bank of the South Bosque
River, 100 yards south of the bridge of the Speegleville road, and 5.5 miles
west of the courthouse at Waco, Texas. Fig. 3, type individual, x 4.0, show-
ing tubercles and angularity of profile. Fig. 7, same individual, x 2.0, show-
ing aperture.
Figure 5. Acanthoceras worthense n. sp Page 93
Abundant, basal and middle Pawpaw clay. Individual showing venter, x 4.0.
Locality: 714, near Fort Worth, Texas.
Figures 8-11. Schloenbachia wintoni n. sp. . . Pag* 90
Occasional, Pawpaw formation; abundant, Weno formation. Figs. 8, 11, type
individual, x 1.0; locality 601, near Gainesville, Texas, nacreous individual
from ironstone in upper third of Weno formation. Figs. 9-10, nacreous indi-
vidual, x 1.0, same locality. Fig. 9 shows the slightly bifid marginal tubercles.
Type in museum of Texas Christian University, Fort Worth, Texas.
University o.' Te as Lulletin No. 1856
Plate 3
PLATE 4
Schloenbachia, Engonoceras, Flickia, Corbula
166 University of Texas Bulletin
PLATE 4.
Schloenbachia Engonocreas, Flickia, Corbula Plate 4
figure 1. Schloenbachla sp
Rare, Pawpaw clay, x 4.0. Locality: 714, near Fort Worth, Texas. (See PI. 1,
fig. 6.)
i
Figure 2. Engonocerai sp Page 85
Rare, Pawpaw clay, x 2.5. Locality: 714, near Fort Worth, Texas.
Figure 4. Acanthocera* wortheiue n. sp Page 93
Abundant, Pawpaw clay, x 4.0. Locality: 714, near Fort Worth, Texas.
Figures 3, 5-6, 12. Engonoceras serpentinum (Cragin) Page 84
Occasional, Weno shale, Grayson and Cooke counties, Texas and southern Okla-
homa; rare, Pawpaw clay and shale. Figs. 3, 5, x 2.5; locality: 714, near
Fort. Worth, Texas. Figs. 6, 12, x 1.0; locality: 604, near Denison, Texas.
Figures 8-10. Engonoceras sp Page 85
Very abundant, Pawpaw clay, especially near the base; rare, Grayson, Denton,
and Duck Creek formations, clay and marl facies, x 3.0, locality: 714, near
Fort Worth, Texas.
Figure 11. Flickia (?) bosquensi* n. sp Page 87
Rare, top of Exogyra arietina horizon, middle Del Rio clay (equivalent of base
of Grayson formation). Type individual, x 4.0. Locality: cliff on west bank
of South Bosque River, 100 yards south of the bridge of the Speegleville road,
and 5.5 miles west of the courthouse at Waco, Texas. (See pi. 1, fig. 4.)
University of Texas Bulletin No. 1856
12
PLATE 5
Hemiaster, Epiaster, Enallaster
158 University of Texas Bulletin
PLATE 5.
Hemiaster, Epiaster, Enallaster Plate 5
Figures 1-2, 4. Hemiaster calvini Clark Page 114
Occasional, Weno and Pawpaw formations; rare, Denton and Mainstreet forma-
tions; abundant, middle Grayson formation. Fig. 1, large sized individual with
strongly developed ambulacral grooves, x 2.0; locality: Argyle, Texas, Gray-
son marl, Baylor University Museum. Fig. 2, individual in some respects re-
sembling Hemiaster bexwi Clark, x 3.0; locality: 720, basal Pawpaw marl,
near Riovista, Texas. Fig. 4, x 2.0; locality: west branch of Little Mineral
Creek, one mile northeast of Fink, Texas.
Figure 3. Enallaster wenoensis n. sp Page 112
Abundant, Weno formation, marl facies; rare, Pawpaw formation, marl and clay
facies. Type individual, x 4.0; locality: 720, basal Pawi.iaw marl, near Rio-
vista, Texas.
Figure 5. Epiaster aguilerae Bose Page 109
Rare, basal Fort Worth limestone. Locality: 406, one-half mile east of Texas
Christian University, Fort Worth, Texas. Aboral side, x 1.0.
Univeriity of Texas Bulletin No. 1856
Plate 5
PLATE 6
Remondia( ?), Venericardia, Amberleya, Hemiaster, E piaster
160 University of Texas Bulletin
PLATE 6.
Remondia, Venericardia, Amberleya, Hemiaster, Epiaster Plate 6
Figure 1. Remondia (?) acuminata (Cragin) Page 136
Occasional, basal Weno marl; rare, Pawpaw clay. Locality: 618, near Fort Worth,
Texas, individual, x 1, showing hinge structure.
Figure 2. Venericardia wenoensis n. sp Page 125
Occasional, Weno formation, shale facies, Red River region, and marl facies,
Fort Worth region. Fig. 2, individual, x 2.0, showing ribbing. Locality: 618,
near Fort Worth, Texas.
Figure 3. Hemiaster calvini Clark Page 114
Occasional, Weno and Pawpaw formations. Fig. 3, x 3.0. Locality: 903, Gray-
son marl, one-half mile southeast of Denison, Texas.
Rare, basal Pawpaw formation, clay-marl transition area; rare, Weno marl.
Type individual, x 4.0. Locality: 720, near Riovista, Texas.
Figure 4. Hemiaster riovistae n. sp Page 115
Rare, Weno formation, shale facies. Locality: 606, basal stratum of Weno form-
ation, near Denison, Texas. Type individual, x 2.0, showing carinae and
ribbing.
Figure 5. Amberleya graysonensis n. sp Page 137
Abundant, basal Weno formation, marl facies; rare Pawpaw clay and marl.
Type individual, x 1.0. Locality: 618, near Fort Worth, Texas.
Figure 6. Epiaster wenoensis n. sp Page 105
Abundant, basal Weno formation, marl facies; rare, Pawpaw clay and marl.
Type individual, x 1.0. Locality: 618, near Fort Worth, Texas.
University of Texas Bulletin No. 1856
Plate 6
PLATE 7
Pentaceros, Comptonia, Metopaster, Pentagonaster
162 University of Texas Bulletin
PLATE 7
Pentaceros, Comptonia, Metopaster, Pentagonaster Plate 7
Figures 1-3. Pentaceros americanus n. sp Page 99
Pawpaw formation, clay facies, basal 5 feet, rare.
Fig. 1. Type individual, aboral side, x 2. Locality: 714, one-fourth mile south
of the International and Great Northern Railway bridge across Sycamore
Creek, four and one-half miles southeast of Fort Worth, Texas. The large
~ plate above and to the left of the center of the disk is the madreporite. Type
in museum of Texas Christian University, Fort Worth, Texas.
Fig. 2. Type individual, oral side, x 2.
Fig. 3. Type individual, aboral side, x 1.5.
Figures 4-5. Comptonia wintoni n. sp Page 97
Pawpaw formation, clay facies, basal portion, rare.
Fig. 4. Type individual, aboral side, x 2. Locality: 714, near Fort Worth, Texas.
Fig. B. Type individual, oral side, x 2.
Figure 6. Metopaster hortensae Adkins and Winton Page 97
Pawpaw formation, clay facies, base, rare.
Type individual, oral side, x 2. Locality: 714, near Vort Worth, Texas.
Figure 7. Pentagonaster texensis Adkins and Winton Page 95
Weno formation, limestone facies, upper 10 feet, rare
Locality: 602, east bank of Sycamore Creek, about four miles Southeast of Fort
Worth, Texas. Aboral side, x 1.5. Figured individual in museum of Texas
Christian University, Fort Worth, Texas.
University of Texas Bulletin No. 1856
Plate 7
V
164 University of Texas Bulletin
PLATE 8.
Hemiaster, Epiaster, Enallaster. Plate 8
Figure 1. Hemiaster longisulcus (Adkins and Winton)
Occasional, top of Fort Worth limestone. 1/pe individual, x 2.0. Locality: On
Cedar Creek, two miles southeast of Blum, Texas. Note the similar pores of
the anterior unpaired ambulacrum, and the posteriorly placed apical system.
Figures 2-3, 5. Hemiaster riovistae n. sp Page 115
x 2.0. Locality: 720, near Riovista, Texas.
Figure 4. Enallaster bravoensis Bosc Page 114
Occasional, Weno formation, marl and clay facies; rare, Pawpaw, Mainstreet and
Buda formations; abundant, Grayson formation, marl and clay facies. Fig. 4,
individual x 2.0. Locality 618, near Fort Worth, Texas.
Figure 6. Hemiaster calvini Clark Page 114
Locality unknown, Cummins Collection. Note position of apical system, and the
deep ambulacra! grooves.
Figure 7. Epiaster aguilerae Bose Page 109
Rare, basal Fort Worth limestone. Locality: 406, one-half mile east of Texas
Christian University, Fort Worth, Texas. (Same individual as PL 5, fig. 5.)
Apical system, x 4.0.
University of Texas Bulletin No. 1856
Plite 8
PLATE 9
Cyprimeria, Corbula
166 University of Texas Bulletin
PLATE 9.
Cyprimeria, Corbula Plate 9
Figures 1-6. Cyprimeria washitaensis n. sp Page 134
Occasional, Weno shale, Cooke and Grayson counties, Texas Fig. 1, type indi-
vidual, x 1.0; locality: 604, near Denison, Texas. Figs. 2-4, x 1.0, same locality.
Figs. 3-5, individuals showing hinge structure, x 1.0, same locality. Fig. 6,
individual showing posterior adductor muscle scar and part of pallial line,
x 1.0, same locality.
Figures 7-24. Corbula basiniformU n. sp Page 130
Abundant, Weno shale and ironstone. Cooke and Grayson counties, Texas and
southern Oklahoma. Fig. 21, type individual, x 1.5; locality: 604, near Den-
ison, Texas. Other individuals, x 1.5, same locality.
University of Texas Bulletin No. 1856
Plate 9
20
PLATE 10
Corbula, Area, Protocardia, Neritina, Nerita, Natica, Lunatia,
Trochus, Anchura, Cinulia, Globiconcha, Turritella
168 University of Texas Bulletin
PLATE 10.
Corbula, Nucula, Area, Protocardia; Neritina, Nerita, Natica, Lunatia, Plate 10
Trochus, Anchura, Cinulia, Globiconcha, Turritella
Figures 1-4. Corbula wenoeiuU n. sp Page 127
Weno shale, rare. Fig. 4, type. All individuals x 1.5. Locality: 601, pit of
brickyards, one and three-fourths miles southeast of Gainesville, Texas.
Figure 5. Corbula littoralis n. sp : Page 133
Weno shale, rare. Fig. 5, type individual, x 1.5. Locality: 601, pit of brick-
yards, one and three-fourths miles southeast of Gainesville, Texas.
Figure 6. Area wasbitaensi* n. sp Page 121
Abundant, Pawpaw clay; rare, Grayson, Den ton and Duck Creek formations, clay
facies and more rare in the marl facies. Fig. 6, type individual, x 1.5.
Locality: 714, one-fourth mile south of the International and Great Northern
Railway bridge across Sycamore Creek, near Fort Worth, Texas, at the base
of the Pawpaw clay.
Figures 7-9. Corbula basiniformis n. sp Page 130
Abundant, Weno shale. Locality: 604, cut of St. Louis and San Francisco Rail-
way, one mile north of Union Station, Denison, Texas. (See PI. 9, figs. 7-24.)
x 1.5.
Figures 10111. Nucula wenoentis n. sp Page 120
Rare, Weno shale. Fig. 10, type individual, x 1.5. Fig. 11, x 1.5. Locality: 601,
pit of brickyards, one and three-fourths miles southeast of Gainesville, Texas.
Figures 12-16, 19-20. Nucula nokonu n. sp Page 118
Occasional, Weno shale, x 1.5. Locality: 604, near Denison, Texas. Type, Fig.
19, x 1.5, same locality.
Figures 21-26, 32. Protocardia sp. aff. multistriata (Shumard) Page 126
Abundant, Weno ironstone and shale, x 1. Locality: 601, near Gainesville, Texas.
Figure 27. Neritina sp Page 139
Rare, middle Weno shale (buff marl). Locality: 601, near Gainesville, Texas.
xl.5.
Figure 28. Nerita sp Page 139
Rare, middle Weno shale. Locality: 601, near Gainesville, Texas, x 1.5.
Figure 29. Natica sp Page 140
Rare, ironstone and upper Weno shale. Locality: 601, near Gainesville, Texas.
Weno and Pawpaw Formations 169
Figures 30-31. Trochu* laticonicut n. sp. . Page 138
Rare, middle Weno shale (buff marl). Locality: 601, near Gainesville, Texas.
Fig. 30, type individual, x 1.6. Fig. 31, x 1.5.
Figures 33-37. Cinulia washitaensii n. sp Page 143
Occasional, middle and upper Weno shale. Locality: 601, near Gainesville, Texas.
Fig. 33, type individual, x l.B. Figs. 34-37, x 1.5.
Figure 38. Lunatia sp Page 140
Rare, Weno ironstone and upper Weno shale. Locality: 601, near Gainesville,
Texas. x 1.5.
Figures 39-40. Ancjiura mudgeana White Page 139
Abundant, middle and upper Weno shale, Cooke and Grayson counties, Texas.
Locality: 604, near Denison, Texas, x 1.5.
Figure 41. Globiconcha sp Page 140
Rare, Weno ironstone. Locality: 601, near Gainesville, Texas, x 1.5.
Figure 42. Turritella worthensis n. sp Page 142
Abundant, lower Weno marl, Tarrant County, Texas. Type. Locality, 618, near
Fort Worth, Texas. Fig. 42, type invidual, x 1.5.
Figure 43. Turritella grayioneniis n. sp Page 140
Abundant, Weno shale, Grayson County, Texas; occasional, Cooke County, Texas.
Locality: 604, near Denison, Texas. Type, Fig. 43, x 1.5.
University of Texas Bulletin No. 1856
Plate 10
39
PLATE 11
Pecten, Epiaster, Nodosaria, Ancycloceras
172 University of Texas Bulletin
PLATE 11.
Pecten, Epiaster, Nodosaria, Ancycloceras. Plate 11
Figure 1. Ancycloceras bendirei n. sp Page 70
Rare, Weno formation, base, marl facies. Fig. 4, type individual, x 1.2. Locality:
618, near Fort Worth, Texas.
Figure 2. Nodosaria texana Conrad Paije 145
Abundant as isolated individuals and rarely in slabs, upper third of Weno and
base of Pawpaw formations in north central Texas; abundant in flag layers,
upper and to a less extent the middle Del Rio clay in West Texas. Fig. 3,
x 5.0. Locality: Terlingua, Texas. (Compare Univ. Texas Bull 1945, pi. 21.)
Figure 3. Epiaster subobesus n. sp Paga 110
Occasional, Weno formation, marl facies, and Pawpaw formation, marl facies.
Abundant near base of Weno, in the "first terrace" of the Fort Worth region.
Fig. 2. Locality: 618, near Fort Worth, Texas, type individual, x 1.0.
Figure 4. Pecten inconspicuus Cragin Page 12.3
Abundant, Weno shales and ironstone; rare, Denton clay; rare, Pawpaw forma-
tion, sand and ironstone facies. Cooke and Grayson counties, Texas, and
southern Oklahoma. Fig. 1, clay-ironstone shell conglomerate from the middle
Weno shales, x 4.0. Locality: 604, near Denison, Texas.
University of Texas Bulletin No. 1856
• . .'
On A New Ammonite Fauna of the Lower Turonian
of Mexico
BY
Emil Bbse
176 University of Texas Bidletin
Exogyra Say 230
Exogyra haarmanni sp. nov 230
Exogyra of r. olisiponensis Sharpe 230
GASTROPODA 232
Tylottoma Sharpe 232
Tylostoma aff . ovatum Sharpe 232
• ECHINODERMATA 232
Hemiaster Desor 232
Hemiaster sp 232
LIST OF ILLUSTRATIONS
FIGURES
Figure 1. Metoecocerai aff. white! Hyatt, suture 204
Figure 2. Suture, Vatcocera* angermanni «i. sp. (above) and Vascocerat aff.
adonense Choffat (below) 216
Figure 3. Suture, Va.cocera. aff. gamai Choffat 21G
Figure 4. Sutures, Vascocera* mohovanenie n. sp. (above) , and Mammite*
mohovaensi* n. sp. (below) 220
Figure 5. Suture, Neoptychite* aff. cephalotu* Courtiller 222
Figure 6. Suture, Neoptychite* aff. cephalotu.- Courtiller 222
Figure 7. Sutures, Neoptychite* aff. xetriformU Pervinquiere (lower left hand
corner) and Hoplitoide* sp. (other three) 226
PLATES
Plates 12-20. Lower Turonian Fossils from Cerro del Macho.. ..235-252
ON A NEW AMMONITE FAUNA OF THE LOWER TURONIAN
OF MEXICO
BY EMIL BOSE
I
INTRODUCTION
A number of years ago the existence of Turonian beds was proven in
Mexico and later on it was shown that these beds have a great distribu-
tion in the country. At first very few localities with faunas of this age
were known, but later the finds of fossils of Turonian age have augmented
in such a manner that we now know that the Turonian has a vast dis-
tribution in Mexico, numerous localities having been discovered between
Lat. 20°30' N. and Lat. 32° N. All of these beds are petrographically
very uniform and consist of argillaceous shales and laminated limestones
with intercalations of thin beds of limestone, all of black to light gray
color. The fauna of these beds is also rather uniform and consists mostly
of numerous specimens of Inoceramus labiatus Schlotheim, in some places
accompanied by Inoceramus hercynicus Petraschek ; in some localities fishes
are relatively numerous ; in others bivalves other than Inoceramus are
found. Cephalopods have been found very rarely, all of them crushed
and nearly indeterminable. The determination of the age had to be
founded exclusively on the Inoceramus and on the position of the beds
in relation to the Senonian and the Cenomanian.
About nine years ago I received the first collections of Turonian am-
monites, which allowed a much better determination of the age of the
beds mentioned here because these cephalopods were found together with
well preserved specimens of the same Inoceramus which already had been
determined by us as 1. labiatus.
In February, 1911, Dr. Ernst Angermann sent me a email collection
of fossils collected by him on the Cerro del Macho, Hacienda del Moh6vano,
Municipality of San Pedro, District of Parras in the State of Coahuila.
The greater part of these fossils consisted of internal molds of bivalves
and gastropods, but there were also present three cephalopods relatively
badly preserved and several indeterminable fragments of ammonites. I
recognized at once that these fossils belonged to a facies and a horizon
altogether unknown in Mexico, one of the ammonites being a Vascoceras
of the group of V. Kossmati and another a Neoptychites of the group of
N. xetriformis Pervinquiere, the bivalves belonged mostly to Trigoniu,
180 University of Texas Bulletin
Avicula of the group of A. gravida Coquand, the gastropods to Tylostoma
and similar genera.
A short time afterwards I showed these fossils to Dr. E. Haarmann,
geologist of the Cia. Perforadora Mexicana, who then told me that he had
a much larger collection of fossils from the same locality which he had
made before Dr. Angermann had visited the place ; and he offered me his
material for a detailed paleontological study. The collection of Dr. Haar-
mann proved to be much larger than that of Dr. Angermann and con-
tained a large number of ammonites some of which were rather well
preserved. Haarmann in making his collection had separated the fos-
sils of the different beds. The lowest of these beds was represented by
a single piece of rock with impressions of bivalves, but as this rock had
a very distinct character from that of the other beds and as in a locality
of apparently the same age a badly preserved sea urchin had been found
which appeared to belong to Hemiaster, I asked Dr. Haarmann to collect
better material in the lowest horizon, because this horizon seemed to be-
long to the Cenomanian. Haarmann visited the locality again in August,
1911, collected ammonites in each of the three beds distinguished by him,
and turned this material over to me in April, 1912.
The material thus collected proved to be of great stratigraphical and
paleontological interest, as will be shown by the following description.
But before I enter into a detailed study I wish to express my gratitude
to Dr. E. Haarmann to whose amiability I owe the opportunity of studying
this interesting fauna. I also wish to express my obligations to Professor
Dr. W. Branca in Berlin who kindly sent me a great number of photo-
graphs of Turonian ammonites from Egypt, studied by Dr. Eck but at
that time still undescribed.
LIST OF LITERATURE CITED IN THIS PAPER
1. Boule, Lemoine et Thevenin, Diego Suarez. — M. Boule, P. Lemoine et A. Thevenin,
Paleontologie de Madagascar. Cephalopodes cretaces des environs de Diego-
Suarez. — Ann. de Palontologie t. I et II, Paris, 1906-07.
2. Choffat, Especes nouv. ou peu conn. — P. Choffat, Recueil d'etudes paleontologiques
sur la faune cretacique du Portugal. Vol. L, Especes nouvelles ou peu
connues. Ire. serie. Section des Travaux geologiques du Portugal. Lisbon,
1886.
3. Choffat, Syst. cret. Portugal II. — P. Choffat, Recueil de Monographies strati-
graphiques sur le systeme cretacique superieur au nord du Tage. Service
geol. du Portugal. Lisbonne, 1900.
4. Chudeau, Ammonites du Damergou. — R. Chudeau, Ammonites du Damergou
(Sahara meridional). — Bull. Soc. geol. France, 4me ser., t. 9, fasc. 1-2, 1909.
5. Coquand, Geol. et Pal. de Constantine. — H. Coquand. Geologic et Paleontologie
de la region sud de la Province de Constantine. Mem. Soc. d'Emulation de
la Provence, II. Marseille, 1862.
A New Ammonite Fauna of the Lower Turanian of Mexico 181
6. Cotteau, Peron et Gauthier, Ech. foss. de 1'Algerie. — Cotteau, Peron et Gauthier,
Echinides fossiles de 1'Algerie. Description des especes deja recueillies das
ce pays et considerations sur leur position stratigraphique. IV, Etage Ceno-
manien. Paris, 1878.
7. Eck, Turon in Aegypten. — O. Eck, Vorlaufige Mitteilungen tiber die Bearbeitung
der Cephalopoden der Schweinfurthschen Sammlung und Uber die Entwick-
lung des Turons in Aegypten. Monatsber. d. Deutsch. Geol. Ges. 1910. Ber-
lin, 1911.
8. Fourtau, Faune cret. d'Egypte. — R. Fourtau, Contribution a 1'etude de la faune
cretacique d'Egypte. Bull. Institut Egyptien, ser. 4, vol. 4, 1903.
9. Fritsch, Ceph. bohm. Kreideform. — A. Fritsch, Cephalopoden der bohmischen
Kreideformation (unter Mitwirkung des Dr. Urb, Schlonbach). Prag, 1872.
10. Geinitz, Elbthalgebirge. — H. Br. Geinitz, Das Elbthalgebirge in Sachsen. Pala-
eontographia Bd. 20, I u. II. 1872-75.
12. Gueranger, Album Paleontol. — Ed. Gueranger, Album Paleontologique de la
Sarthe representant au moyen de la photographic les fossiles recueillis dans
cette circinscription. Le Mans, 1867.
13. Guillemain und Harbort, Profil d. Kreidesch. a. Mungo. — C. Guillemain und E
Harbort, Profil der Kreideschichten am Mungo. Abh. d. k. Preuss. Geol.
Landesanstalt Neu Folge, Heft 62, 1909.
14. Haug, Traite de Geologic. Paris, 1908-11.
16. Hyatt, Pseudocer. — A. Hyatt, Pseudoceratites of the Cretaceous. Edited by T. W.
Stanton. U. S. Geol. Surv. Monogr. vol. 44, Washington, 1903.
16. Jack and Etheridge, Queensland.— R. L. Jack and R. Etheridge, Jr. The Geology
and Paleontology of Queensland and New Guinea. Brisbane and London
1892.
17. v. Koenen, Nachter. Foss. Mungo in Kamerun. — A. von Koenen, Nachtrag zu
Ueber Fossilien der Unteren Kreide am Ufer des Mungo in Kamerun. Abh.
K. Ges. d. Wiss. zu Gottingen, Math. Phys. Kl. Neue Folge, Bd. 1, No. 1
1898.
18. Kossmat, Stidind. Kreideform. — Fr. Kossmat, Untersuchungen uber die sudin-
dische Kreideformation. Beitrage zur Palaeontologie und Geologie Oester-
reich-Ungarns und des Orients, I Bd. 9, 1895; II u. Ill Bd. 11, 1897.
19. Lartet, Geol. de la Palestine.— L. Lartet, Essai sur la geologie de la Palestine
et des contrees avoisinantes telles que 1'figypte et PArabie. II me partie
Paleontologie. Ann. d. Sciences Geologiques publ. s. 1. dir. de M. Hebert et
A. Milne-Edwards. T. III. Paris, 1872.
20. Laube und Bruder, Amm. d. bohm. Kreide.— G. C. Laube und G. Bruder, Ammo-
nites der bohmischen Kreide. Palaeontographica Bd. 33, 1887.
21. Lisson, Amm. del Peru. — C. I. Lisson, Contribucion al conocimiento sobre algunos
Ammonites del Peru. 4o Congreso cientifico Latino-Americano, lo Panamer-
icano, celebrado en Santiago de Chile. Lime, 1908.
22. Lisson, Terr, recon. en el Peru.— C. I. Lisson, Terrenes reconocidos hasta hoy
en el Peru y sinopsis de su fauna y flora fosiles. Bol. de Minas, Ind. y Constr
publ. por la Escuela de Ingenieros, ser. II, t. IV. Lima, 1912.
23. Peron, Amm. du Cret. sup. de 1'Algerie. — A Peron, Les ammonites du Cretace
superieur de 1'Algerie. Mem. Soc. geol. France, Paleontologie, t. 6 et 7
mem. no. 17. 1896-97.
24. Pervinquiere, fit. geol. Tunisie.— L. Pervinquiere, Etude geologique de la Tunisie
182 University of Texas Bulletin
Centrale. Theses presentees a la Faculte des Sciences de Paris p. obt. le
grade de Docteur-es-Sciences Naturellea. Paris, 1903.
25. Pervinquiere, Paleontologie Tunisienne. — L. Pervinquiere, fitudes de Paleontologie
Tunisienne. I Cephalopodes des Terrains Secondaires. Dir. Gen. des Travaux
Publics, Carte geol. de la Tunisie. Paris, 1907.
26. Petrascheck, Amm. d. sachs. Kreideform. — W. Petrascheck, Die Ammoniten der
sachsischen Kreideformation. Beitr. z. Pal. u. Geol. Oesterreich-Ungarns u. d
Orients. Bd. 14, 1902.
27. Petrascheck, Inoc. a. d. Kr. Bohmens. — W. Petrascheck, Ueber Inoceramen aus
der Kreide Bohmens und Sachsens. Jahrb. d. K. K. Geol. Keichsanstalt. Wien
Bd. 53, 1903 (1904).
28. Roemer, Kreidebild. v. Texas. — F. Roemer, Die Kreidebildungen von Texas und
ihre organischen Einschliisse. Bonn, 1852.
29. Schlagintweit, Vracon u. Cenoman in Peru. — 0. Schlagintweit, Die Fauna des
Vracon und Cenoman in Peru. N. Jahrb. f. Min., Geol. u. Pal., Beilagebd.
33, 1912.
30. Sharpe, Secondary distr. of Portugal. — D. Sharpe, On the Secondary District
of Portugal which lies on the North of the Tagus. Quart. Jour. Geol. Soc
London, Vol. VI, 1850.
31. Sharpe, On Tylostoma. — D. Sharpe, On Tylostoma, a proposed genus of Gaste-
ropodous Mollusks. Quart. Jour. Geol. Soc. London, Vol. 4, 1849.
32. Solger, Mungokreide. — Fr. Solger, Die Fossilien der Mungokreide von Kamerun
und ihre geologische Bedeutung, mit besonderer Beriicksichtigung der Am
moniten. Beitrage zur Geologic von Kamerun herausgeg. v. E. Esch. Stutt-
gart, 1904.
33. Stanton, Colorado Form.- — T. W. Stanton, The Colorado Formation and its in-
vertebrate Fauna. U. S. Geol. Surv. Bull. No. 16, 1893.
34. Stoliczka, Ceph. Cret. Rocks India. — F. Stoliczka, The fossil cephalopoda of the
Cretaceous Rocks of Southern India (Ammonitidae). Mem. of the Geolog-
ical Surv. of India. Palaeontologia Indica, 1865.
35. Thomas et Peron, Hauts-Plateaux de la Tunisie. — Ph. Thomas et A. Peron
Description des mollusques fossiles des Terrains Cretaces de la region sud
des Hautes — Plateaux de la Tunisie recueillis en 1885 et 1886. Exploration
Scientifique de la Tunisie. Paris, 1889-90.
36. White, Inv. foss. Nevada, Utah, etc. — Ch. A. White, Report upon the inverte-
brate fossils collected in portions of Nevada, Utah, Colorado, New Mexico,
and Arizona, by parties of the expeditions of 1871, 1872, 1873 and 1874.
Report upon Geogr. and Geol. Expl. and Surv. west of the 100th Meridian by
Geo. A. Wheeler. Eng. Dept. U. S. Army, Part IV Palaeontology. Wash-
ington, 1875.
37. White, Brazil. — Ch. A. White, Contributes a Paleontologia do Brazil. Archives
do Museu Nacional do Rio de Jeneiro, Vol. VII, 1887.
38. Woods, Cret. dep. Northern Nigeria. — H. Woods, The palaeontology of the upper
Cretaceous deposits of Northern Nigeria. The Geology and Geography of
Northern Nigeria by J. D. Falconer. London and Bungay, 1911.
39. Yabe, Cret. Ceph. Hokkaido II. — H. Yabe, Cretaceous Cephalopoda from the
Hokkaido. Part II. Jour, of the College of Science, Imp. Univ., Tokyo,
1904, Vol. 20, art. 2.
A New Ammonite Fauna of the Lower Turanian of Mexico 183
40. Yabe, Strat, u. Pal. Hokkaido.— H. Yabe, Zur Stratigraphie und Palaontologie
der oberen Kreide von Hokkaido und Sachalin. Zeitschr. d. Deutsch. geol.
Ges. Bd. 61, 1909.
41. Zittel, Lib. Wiiste. — K. A. Zittcl, Beitrage zur Geologie und Palaeontologie der
Libyschen Wiiste und der angrenzenden Gebiete von Aegypten. I. Geolo-
gischer Theil. Palaeontographica Bd. 30, I. 1883.
STRATIGRAPHY
The Cerro del Macho is a small hill in the eastern part of the Hacienda
del Mohovano belonging to Mr. Frederick Ritter. The hacienda lies to the
southeast of the station Carillo of the railway which connects Sierra Mo-
jada, Coahuila with Escalon, Chihuahua (Mexican Central Railway) and
part of its land belongs to the State of Chihuahua while the rest lies in the
State of Coahuila. The Cerro del Macho belongs to this last region and
lies near the boundary line of both states.
Dr. E. Haarmann gave me the following geological cross-section of the
fossiliferous locality, to which I add the stratigraphical explanation ob-
tained as the result of the study of the fauna.
-JT
Fig. 1
Fossil bearing beds on the Cerro del Macho, Hacienda del Moh6vano,
Coahuila.
III. Gray hard limestones "1
II. Gray-bluish marls J
I. Yellow and red marls and argillaceous limestones Upper Cenoman-
Lower Turonian.
Three different petrographical horizons can be distinguished : the low
est beds consist of yellow and red marls with argillaceous limestones con-
taining numerous fossils, especially bivalves; this horizon which for the
present we shall designate with the number I has a thickness of only two
184 University of Texas Bulletin
meters in this locality, but its base is covered. Above these marls lie gray-
bluish marls with large cephalopods ; the thickness of this horizon which
we designate as Number II, is 2.5 meters. On top of these marls we find
gray limestones with numerous cephalopods, bivalves and gastropods ; the
thickness of this horizon, which we call Number III, is about 5 to 6 meters,
its upper limit being unknown. According to Dr. Haarmann the beds
show a strike of N50-60°E and a dip of approximately 10°NW.1
The whole outcrop has thus only a thickness of about 10 meters, but
nevertheless we find two different horizons, as will be shown in the
following. Among the fossils collected in this locality I have been able to
distinguish twenty-one different species which are distributed in the three
horizons in the following manner :
Horizon I.
Metoecoceras aff. Whitei Hyatt
Metoecoceras n. sp.
Exogyra Haarmanni n. sp.
Exogyra cfr. olisiponensis Sharpe
Hemiaster sp.
Horizon II.
Mammites mohovanensis n. sp.
Pseudaspidoceras aff. Footeanum Petrascheck
Pseudaspidoceras aff. pedroanum White
Vascoceras aff. Adonense Choffat
Fagesia Haarmanni n. sp.
Fagesia Pervinquieri n. sp.
Horizon III.
Vascoceras Angermanni n. sp.
Vascoceras ex. aff. Gamai Choffat
Vascoceras (?) sp.
Vascoceras mohovanense n. sp.
Neoptychites aff. xetriformis Pervinquiere
Hoplitoides aff. mirabilis Pervinquiere
Inoceramus labiatus Schlotheim
Avicula Aguilerae n. sp.
Trigonia sp.
Crassatella sp.
Tylostoma aff. ovatum Sharpe
To show the stratigraphic importance of the different species we shall
have to compare them with related forms.
iAccording to a sketch of Dr. Angermann the strike of the beds i3 N-S and the
dip 10 degrees W.
A New Ammonite fauna of the Lower Turanian of Mexico 185
Horizon I.
Upper
Cenomanian Turonian
Species from Cerro del Macho Related species
Metoecoceras aff. Whitei Hyatt M. Whitei Hyatt ? T
Metoecoceras n. sp. M. Geslianum Petrascheck +
Exogyra Haarmanni n. sp.
Exogyra cfr. olisiponensis Sharps Ex. olisiponensis Sharpe + +
Hemiaster sp.
The age of this horizon cannot be determined quite exactly. The fossils
are few, the cephalopods among them indicate only that the horizon belongs
either to the lower Turonian or the upper Cenomanian. Metoecoceras aff.
Whitei is similar to forms found in the Colorado Formation of the United
States, a division which up to now has not been subdivided stratigraphic-
ally with the necessary exactness ; it probably represents in its larger part
the Turonian, but may possibly contain some upper Cenomanian and a por-
tion of Emscherian. The portion in which M. Whitei has been found be-
longs to the lower part of the formation, which is either the lower Turonian
or the upper Cenomanian. Our Metoecoceras n. sp. is very similar to M.
Geslianum Petrascheck,1 which occurs in the upper Cenomanian of Saxony,
but we do not know exactly if our specimen has been found in this lowest
horizon or in one a little higher.
Interesting is the occurrence of an Exogyra certainly belonging to the
group of Exogyra olisiponensis Sharpe. This species is found on the bor-
der of the Mediterranean in the Cenomanian as well as in the Turonian,
although the variety which is most similar to our specimen seems to be
limited principally to the Cenomanian. Our Exogyra Haarmanni n. sp. is
a new species and not very characteristic, therefore without any strati-
graphic value. The Hemiaster found in the same bed can not be used for
the determination of the age as it does not appear to be identical with any
described species nor to be closely related to any known species which
might indicate the age of these beds.
The small number of fossils of this horizon does not allow an exact de-
termination of its age. Taking into consideration the radical difference be-
tween the character of this fauna and that of Horizon II, and the presence
of a form of Metoecoceras very similar to the one of the upper Cenomanian
of Saxony, I feel inclined to consider this horizon provisionally as upper
Cenomanian until other and more characteristic fossils allow a more exact
determination of the age.
Much more numerous is the fauna of Cephalopods in Horizon II and
iPetrascheck. Amm. d. sachs. Kreideform., 1.140 (10) pi. 7 (1) ; figs. 3-5.
186 University of Texas Bulletin
their forms are so characteristic that they easily allow the determination of
the age of these beds. In the following table we shall compare them with
related species of other countries.
Horizon II.
Turonian
Species from Cerro del Macho Related species Lower Middle
Mammites mohovanensis n. sp. M. nodosoides Schlotheim
Pseudaspidoceras aff. Footeanum P. Footeanum Petrascheck +
Pseudaspidoceras aff. pedroanum P. Footeanum Stoliczka +
Vascoceras aff. adonense V. adonense Choffat +
Fagesia Haarmanni n. sp. F. superstes Kossmat +
Fagesia Pervinquieri n. sp. F. tevesthensis Peron +
All the species of this horizon indicate that it belongs to the lower Tu-
ronian or Salmurian. It s true that Choffat cites his Vascoceras adon-
ense from the middle Turonian, but I believe that this middle Turonian of
Portugal belongs in reality still to the Salmurian, i.e., the lower Turonian.
The occurrence of forms belonging to the groups of Fagesia superstes, Fa-
gesia tevesthensis, Mammites nodosoides, Inoceramus labiatus, etc., ap-
pears to be quite decisive for the determination of the age of those beds.
In our own case we have to consider that this horizon lies immediately
above what we take to be upper Cenomanian ; there seems to be no reason
to doubt that our Horizon II represents the very lowest Turonian. This
idea is confirmed also by the fauna of Horizon III, which will be discussed
farther on.
Our Mammites mohovanensis is very nearly related to M. nodosoides
Schlotheim. It differs principally in its broader cross section; still more
similar to our species is Mammites conciliatus Stoliczka, which belongs to
the same group, the main difference consisting in its more evolute form
and some details of ornamentation. In these details our form is still more
similar to a form determined by Fritsch as Mammites conciliatus which in
reality occupies an intermediate position between our species and that of
India.
The species which we have called Pseudaspidoceras aff. Footeanum Pe-
trascheck is much less related to the type of this group (P. Footeanum
Stoliczka) than to the specimens from the lower Turonian of Saxony de-
scribed by Petrascheck, on account of the more rounded and less subquad-
rangular cross section, as well as the greater height of the whorl. This dif-
ference may be explained in our section by its large size; comparing the
different figured forms of P. Footeanum we see that the adult specimens
tend to lose their quadrangular cross section. This group has been found
A New Ammonite Fauna of the Lower Turanian of Mexico 187
in the lower Turonian in many cases where an exact determination of the
age of the beds has been possible. Varieties of this group have be.en de-
scribed from India, from different parts of northern Africa, as Egypt1
and Tunis- ; from Portugal3, from Nigeria4, from Saxony"', and from Bra-
zil." It is therefore a universally distributed form which characterizes the
lower Turonian.
To the same group of Pseudaspidoceras Footeanum belongs also the
species called by me Pseudaspidoceras an*, pedroanum White. It is still
nearer related to the Indian type than the former species, but differs by
its less strong ribs and the smooth ventral part. In all its characters it is
similar to the Ammonites pedroanus White and only differs in some de-
tails of the ornamentation. The similarity is so great that I have not been
able to separate the two forms specifically and have not united our speci-
men with the Brazilian species only because this latter form is still imper-
fectly known. ' .
Our Vascoreras aff. adonense is certainly very similar to the Portuguese
type from the Turonian, but differs by its suture and the form which is
still more evolute.
The form of greatest stratigraphic interest in our fauna is perhaps our
Fagesia Haarmanni n. sp. It belongs to the group of Fagesia superstes
Kossmat, but differs from the type as well as from all the other species of
this genus by its more evolute form. The species belonging to this group
are limited to the Turonian and especially to the lower part of it. The
type was described from the Utatur group of India,7 and a very typical
form has also been found in Tunis8 ; a nearly related species has been cited
from the Turonian of Portugal.0
Fagesia Pervinqieri n. sp. is a very characteristic species and belongs to
that group of Fagesia which loses its ribs in a rather juvenile state of
growth ; the type of this group is Fagesia tevesthensis Peron. Our species
differs from the type by its higher and less broad whorls. According to
Pervinquiere Fagesia Rudra Stoliczka10 belongs also to this group; this
•Zittel, Lib. Wuste, p. LXXIX (A. cfr. Footeanus) Eck, Turon in Acgypttn. p. 3^0
(Acanthoceras cfr. Footeanum).
2Pervinquiere. Paleontologie Tunisienne, p. 314 (Mammites Salmuriensi*) .
'Choffat, Especes nouv. ou peu conn., p. 66 (Acanthoceras cfr. Foolfanum',
4Woods, Cret. dep. Northern Nigeria, p. 283 (Mam-mites [Pseudaspidocerat] up.)
^Petrascheck, Amm. d. sachs. Kreideform., p. 144 (Mammites f
"White, Brazil, p. 212 (Ammonites pedroanus).
'Kossmat, Sudindische Kreideform., p. 133, pi. 17, fig. 1.
"Pervinquiere, Palecntologie Tunisienne, p. 322, pi. 20, fig. 1-3.
»Choffat, Especes nouv. ou peu conn., p. 69, pi. 10, fig. 4.
'"Stoliczka, Ceph. Cret. Rocks India, p. 122, pi. 60.
188 University of Texas Bulletin
species which occurs in the Utatur group of India is similar to our species
on account of the missing umbilical nodules in a stage of development
which still shows the ribs on the ventral part; it differs, though, by its
much broader and larger whorls. Another form which by Pervinquiere is
considered as belonging to the same group is Ammonites Kotoi Yabe.1 Per-
vinquiere believes that this species is perhaps identical with Fagesia teves-
thensis Peron, but it appears to me that we have here a different species
although it is certainly related to the African form. According to Yabe2
it is not quite certain from which beds this form has been collected ; it oc-
curs either in the Mammites beds or in the Scaphites beds. The age of
Fagesia Rudra is not well known, although Kossmat presumes that this
species belongs to the middle Utatur group. Fagesia tevesthensis charac-
terizes the lower Turonian ; a very similar form exists in beds of the same
age in France and another in the Turonian of Portugal.
Still richer than the fauna of Horizon II is that of the upper limestones
which we have distinguished as Horizon III. For their comparison with
related species we shall again unite them in a table.
Lower
Species from Cetro del Macho Related species Turonian Emscherian
Vascocerat ' tigermanni n. sp. V. Kossmati Choffat +
Vascocera*, ex aff. Gamai V. Gamai, Choffat +
Vascoceras (?) sp. V. (?) arnesense Choffat +
Vascoceras mohovanense n. sp. V. polymorphum Pervinquiere +
Neoptychites aff. cephalotus N. cephalotus Courtiller +
Neoptychites aff. xetriformis N. xetriformis Pervinquiere +
Hoplitoides aff. mirabilis H. mirabilis Pervinquiere +
Inoceramns labiatus Schlotheim /. labiatus Sch'otheim +
Avicula Aguilerae n. sp. A. gravida Coquand + +
Tylostoma aff. ovatum Sharpe T. ovatum Sharpe + (Cenomanian to
upper Turonian
Nearly all of the groups of ammonites cited in this list occur only in the
lower Turonian, to which, according to my opinion, belong also the beds
with Vascoceras of the so-called middle Turonian of Portugal.
Vascoceras Angermanni n. sp. is very similar to V. Kossmati Choffat,
but its form is still a little broader, there is no doubt that it belongs to the
same group and this is until now only known in the Turonian of Portugal
and the lower. Turonian of Egypt.3
The fossil which we have called Vascoceras ex. aff. Gamai Choffat is a
juvenile form and not very well preserved which is very similar to the
iYabe, Cret. Ceph. Hokkaido II, 26, pi. 6, figs. 3-4.
2Yabe, Strat. u. Pal. Hokkaido, p. 441.
3Eck, Turon in Tegypten, p. 381, 382.
A New Ammonite Fauna of the Lower Turanian of Mexico 189
small individuals figured by Choffat1 in figures 3 and 4 of plate 7 and
figure 2 of plate 10. Considering the size and state of preservation this
specimen is not of great stratigraphic value.
Vascoceras (?) sp. is a pretty large specimen which is very similar to
Ammonites arnesensis Choffat. The generic determination is not quite
certain as is also the case with A. arnesensis. Our specimen is a little
twisted ; it does not have much importance for the determination of the
age of the beds.
Vascoceras mohovanense n. sp. is a specimen relatively small but very
characteristic; it belongs certainly to the group of Vascoceras polymor-
phum Pervinquiere of the lower Turonian of Tunis. It differs from the
type by a missing intermediate row of nodules but in its general character
and also in its suture is nearly related to the type. Pervinquiere considers
Vascoceras subconciliatum Choffat from the Turonian of Portugal as a
form of the same group but this species is different from ours on account
of its general form and its suture.
The species described by me as Neoptychites aff. cephalotus Courtiller is
a juvenile specimen which resembles greatly the small individuals of the
cited species, as has been demonstrated in the paleontological part of this
paper. The group of Neoptychites cephalottts characterizes the lower Tu-
ronian ; it occurs frequently in Algiers and Tunis, also in the neighborhood
of Saumur, France. Similar and perhaps identical forms have been found
in India (Neoptychites Telinga Stoliczka)2 and in Kamerun (Neoptychites
Telingaeformis Solger3) ; the aee of the beds where these latter species
have been found is not exactly known.
The form which I compare with Neoptychites xetriformis Pervinouiere,
is not very well preserved but resembles sufficiently the species from Tunis.
Pervinquiere considers as a nearly related form Neoptychites crassus Sol-
ger,4 the age of this latter species is not determined with certainty.
In the limestones of Horizon III we find frequently cephalopods which
resemble very much the bicarinated Hoplitoides of Pervinauiere. The
greater part of these specimens is entirely corroded but in one I have been
able to prepare a portion of the interior whorl which clearly shows the ex-
istence of the two lateral keels on the ventral portion ; one also notes the
suture in part, certainly much destroyed but showing the same elements as
in the bicarinated Hoplitoides. A large specimen has the external form of
'Choffat, Especes nouv. cm peu conn.
2Stoliczka, Ceph. Cret. Rocks India, p. 125, pi. 62; Kossmat, Sudind. Kreideform.,
p. 71, pi. 7, fig. 1, pi. 17, fig. 13.
'Solger, Mungokreide, p. 108.
'Solger, Mungokreide, p. 119, pi. 3, fig. 5.
190 University of Texas Bulletin
Hoplitoides mirabilis but is a little less involute. This group is of some in-
terest in so far as having been found only in the lower and upper Turon-
ian. The types of Hoplitoides mirabilis1 and H. Munieri2 occur in Tunis
mainly in the lower Turonian, H. Munieri also in the upper Turonian. A
similar species has been found also in the Turonian of Egypt.3
In the same Horizon III, Dr. E. Haarmann also collected four specimens
of Inoceramus of which three are typical individuals of Inoceramus labia-
tus Schlotheim. According to an observation made by Jose G. Aguilera,
this fossil occurs in great numbers in beds north of the station of Carillo
which apparently overlie limestones identical with those described here.
In Horizon III occurs very frequently Avicula Aguilerae n. sp. This
species is very similar to Avicula- gravida Coquand which occurs in north-
ern Africa in the Turonian as well as in the lower Senonian or Emscherian.
The form and size of this Avicula are so similar to those of ours that this
find in Mexico has a certain stratigraphic interest.
In the material of Horizon III we find a great number of other bivalves,
but all in the state of internal molds ; a specific determination is entirely
impossible. The most frequent form probably belongs to Tylostoma or
some subgenus of Natica; the greater part of the material is badly pre-
served, but some specimens are a little more complete, although preserved
as internal molds, and resemble strongly Tylostoma ovatum Sharpe which
in Portugal occurs in beds from the Cenomanian to the upper Turonian.
From the character of the fauna of Horizon III we have to conclude that
these beds still belong to the lower Turonian. This appears rather proba-
ble from the circumstance that Horizon II is extremely thin and is well
confirmed especially by the cephalopod fauna. Interesting is the occur-
rence of Inoceramus labiatus Scholtheim. This fossil is extremely common
in Mexico and generally is found in great numbers in calcareous shales
and shaly limestones. The question now is, what relation exists between
those beds and those of Cerro del Macho? In the described locality the
shales, etc., do not exist, but according to the identification of J. G. Aguil-
era these are found north of the station of Carillo where they apparently
overlie limestones similar to those of the Cerro del Macho. If we accept
this explanation, our beds at Cerro del Macho have to be considered as the
lowest part of the Turonian, while the shales with Inoceramus labiatus
would be a little younger and perhaps represent the lower as well as the
upper Turonian. We have no data with which to solve this problem, as up
to now the beds with Inoceramus labiatus have not been found in contact
1Pervinquiere, Paleontologie Tunisienne, p. 218, pi. 10, fig. 3.
2Idem, ibid., p. 217, pi. 10, figs. 1, 2.
3Eck, Turon in Aegypten, p. 380, 386.
A New Ammonite Fauna of the Lower Turanian of Mexico 191
with the cephalopod beds described here ; neither have those beds with Ino-
ceramus labiatus been found in immediate contact with fossiliferous beds
of the Emscherian. Only in one place, Opal, Zacatecas, I have found beds
with Inoceramus labiatus (rare) and /. hercymicus (very frequent) in
contact with sandstones containing an Inoceramus nearly related to Inoce-
ramus cycloides, but the cross section of this locality is too incomplete and
the fauna too poor for a decision of this rather important problem.
The locality of Cerro del Macho is stratigraphically important in so far
as it gives us some data for the limitation of the upper Cenomanian and
the lower Turonian. In a former work we have been able to subdivide the
Cenomanian of Cerro de Muleros near Ciudad Juarez, but we have not been
able to find fossils in the sandstones between the beds with Inoceramus
labiatus and the marls with Hemiaster'Calvini; thus it was impossible to
decide if those sandstones belonged to the Cenomanian or the Turonian.
In the present case we have very fossiliferous beds very near the limit be-
tween the Cenomanian and the Turonian. The fossils of the Cenomanian
are very different from those found up to the present in Cenomanian rocks
of Mexico. Of especial importance is the occurrence of Metoecoceras.
The Turonian ammonite fauna is also entirely new for Mexico, the few
ammonites so far found in the beds with Inoceramus labiatus belonging to
entirely different groups.
Haarmann has distinguished two horizons, II and III, but these do not
appear to be more than local subdivisions notwithstanding the circum-
stance that the fauna of the two beds seem to be rather different. We must
not give too much importance to this circumstance, as the collections so far
made are still rather small and the aspect of the fauna may change alto-
gether with larger collections made. As far as we can see, the lower bed
contains principally cephalopods while in the upper one bivalves and gas-
tropods predominate.
With respect to the conditions of life in this locality we may say with
some certainty that at the end of the CeYiomanian in the Cerro del Macho
region as well as in others of northern Mexico, especially in the State of
Chihuahua, there existed a littoral facies or at least a very shallow sea;
this is indicated by the great quantity of Ostreidae which nearly form beds
or which have been carried away from neighboring beds. At the begin-
ning of the Turonian age the sea seems to have deepened a little, the pre-
dominance of the ammonites and the absence of littoral bivalves indicating
a less shallow sea. It is probable that during the time of the deposition of
the upper part of the Salmurian the sea again became a little shallower;
this is indicated by the predominance of Lamellibranchia and Gastropoda
with thick shells, but the facies is not quite as much a littoral one as in
192
University of Texas Bulletin
Cerro del Muleros near Ciudad Juarez at the same time, where the corre-
sponding beds consist entirely of sandstones.
According to the observations of Haarmann and our palaeontological
studies the stratigraphical cross section of the Cerro del Macho presents
the following features :
5-6 m. of gray limestones with:
Vascoceras Angermanni n. sp., V. ex aff. Gamai Choffat,
Vase, sp., V. mohovanense n. sp., Neoptycliites aff. cepha-
lotus Courtiller, N. aff. xetriformis Pervinquiere, Hopli-
toides aff. mirabilis Pervinquiere, Inoceramus labiatt1?
Schlotheim, Avicula Aguilerae n. sp., Tngonia sp., Cras-
satella sp., Tylostoma aff. ovatum Sharpe, (Lamellibran-
chia and Gastropoda extremely frr-quentj^
Hor. Ill
Lower
Turonian
(Salmurian)
2.5 m. of gray-bluish marls with:
Mammites mohovanensis n. sp., Pseudaspidoceras arf
Footeanum Petrascheck, Ps. aff. pedroanum White, Vasco-
ceras aff. adonense Choffat, Fagesia Haarmanni n. sp
F. Perviniquieri n. sp.
Hor. II
2 m. yellow and reddish marls and limestones with:
Metoecoceras aff. Whitei Hyatt, Meto?.co-;eras nov. sp.,
Exogyra Haarmanvi n. sp., Ex. cfr. disiponensis Sharpe
Hemiaster sp. (Lamellibranchia predominate).
Hor. I
Upper
Cenomanian
If really the beds with Inoceramus labiatus lie immediately on top of the
cephalopod beds, as the observations of J. G. Aguilera seem to indicate,
another deepening of the sea may have followed and the general rising
of the bottom of the ocean did not begin before the age of the lower Se-
nonian.
ON THE RELATIONS BETWEEN THE FAUNA OF CERRO DEL
MACHO AND ISOCHRONOUS FAUNAS OF OTHER REGIONS
OF THE EARTH
The fauna of the upper Cenomanian of Cerro del Macho is too small
to be compared with others ; the most important fossil, Metoecoceras n. sp.
belongs to a group which has been found in the upper Cenomanian. Of
certain interest is the occurrence of Exogyra cfr. olisiponensis Sharpe be-
cause it indicates a faunistic similarity with the development of the Ceno-
manian along the border of the Mediterranean, a circumstance which to a
certain degree can be noted also in the fauna of other Cenomanian beds
of Mexico.
A New Ammonite Fauna of the Lower Turanian of Mexico 193
I
The fossils of the lower Turonian or Salmurian of the Cerro del Macho
present a much better material for faunistic comparisons. Already while
comparing our species with related ones from other regions we have seen
that similar forms are found mainly around the Mediterranean, inclusive
of Portugal. Comparing the faunas of the Salmurian in the above men-
tioned region, we find that all of them contain certain elements which
either do not exist in most other regions or which occur only very rarely
there. We shall see later on that this special fauna is not restricted to
the Mediterranean but extends also to other parts of Africa and that
certain elements belonging to it occur also in Asia and America. This
indicates a large extension of the same horizon, but1 at the present time
it is impossible to say if this distribution coincides with that of the same
paleontological facies. But before we enter into such a discussion we must
compare our fauna with the isochronous faunas of the Mediterranean and
other parts of the earth in a somewhat more detailed manner.
Portugal: We begin with the region of Portugal. According to Choffat1
we find in the lower part of the Turonian (beds with Ostrea columba
major) the following cephalopods:
Puzosia cfr. planulata Sowerby
Vascoceras Mundae Choffat
Vascoceras Gamai Choffat
Pseudaspidoceras cfr. Footeanum Stoliczka
Neolobites sp. nov.
In his middle Turonian we find the following species:
Vascoceras Gamai Choffat
Vascoceras Gamai Choffat var. triangularis Choffat
Vascoceras Mundae Choffat
Vascoceras amieirense Choffat
Vascoceras silvanense Choffat
Vascoceras adonense Choffat
Vascoceras Grossouvrei Choffat
Vascoceras Barcoicense Choffat
Vascoceras Douvillei Choffat
Vascoceras subconciliatum Choffat
Vascoceras harttiforme Choffat
Vascoceras Kossmati Choffat
Vascoceras ( ?) arnesense Choffat
iChoffat, Syst. cret. Portugal II. p. 162, 170, 173.
Choffat, Especes nouv. ou peu conn., p. 44, 47.
194 University of Texas Bulletin
Mammites pseudonodosoides Choffat
Pseudaspidoceras cfr. Footeanum Stoliczka
Fagesia aff. superstes Kossmat
Fagesia aff. tevesthensis Peron
Puzosia cfr. Gaudama Forbes
Puzosia sp.
Pachydiscus peramplus var. beyrense Choffat
Pseudotissotia Barjonai Choffat
Ammonites cfr. Pachydiscus Rollandi Peron
Ammonites sp. ind.
From the upper Turonian the author cites:
Vascoceras Gamai Choffat
Schloenbachia ?
Algeria: The Salmurian in northern Africa, especially in Algeria, Tunis
and Egypt is very well developed. Still, in the year of 1904, Solger1
could not cite from Algeria more than the following species of cephalopods :
According to Peron :
Acanthoceras deverioide Grossouvre
Sphenodiscus Requiem d'Orbigny (Hoplitoides ingens according to
Pervinquiere)
Pachydiscus peramplus Mantell and other species of the same genus
Neoptychites Telinga Stoliczka (N. cephalotus according to Per-
vinquiere)
Puzosia Austeni Sharpe
According to Coquand:
Amm. Fleuriausi d'Orbigny
Amm. papalis d'Orbigny
Hetet -ammonites ammoniticeras Coquand (Hemitissotia Morreni
Coquand according to Pervinquiere)
Peron cites further the following species:2
Mammites ? tevesthensis Peron (=Fagesia tevesthensis according
to Pervinquiere)
Pachydiscus Durandi Thomas et Peron (^Vascoceras Durandi ac-
cording to Pervinquiere)
Pachydiscus Rollandi Peron (=Thomasites Rollandi according to
Pervinquiere)
Tunis: In the present time we owe to the painstaking investigations
of L. Pervinquiere a much more complete knowledge of the fauna of the
iSolger, Mungokreide p. 203.
2Peron, Amm. du Cret. sup. de 1'Algerie.
A New Ammonite Fauna of the Lower Turanian of Mexico 195
Salmurian in northern Africa, especially of Tunis. Pervinquiere cites
and describes the following cephalopods:
Puzosia Austeni ? Sharpe
Pachydiscus peramplus Mantell
Hoplitoides Munieri Pervinquiere
Hoplitoides mirabilis Pervinquiere
Prionotropis Neptuni Geinitz
Acanthoceras Douvillei Pervinquiere
Mammites nodosoides Schlotheim
Pseudaspidoceras salmuriense Courtiller
Pseudaspidoceras armatum Pervinquiere
Fagesia superstes Kossmat
Fagesia tevesthensis Peron
Fagesia Peroni Pervinquiere
Fagesia Fleuryi Pervinquiere
Vascoceras Durandi Thomas et Peron
Vascoceras cfr. barcoicense Choffat
Vascoceras polymorphum Pervinquiere
Thomasites Rollandi Peron
Thomasites Meslei Pervinquiere
Thomasites Jordani Pervinquiere
Pseudotissotia segnis Solger
Pseudotissotia Pavillieri Pervinquiere
Pseudotissotia Luciae Pervinquiere
Pseudotissotia Massipiana Pervinquiere
Neoptychites cephalotus Courtiller
Neoptychites xetriformis Pervinquiere
Neoptychites Courguechoni Pervinquiere
Egypt: Until a very few years ago our knowledge of Turonian faunas
of Egypt was rather fragmentary, but in 1911 Eck published a prelim-
inary study1 of the collections made by Schweinfurth which contain faunas
of the Cenomanian, Turonian and Senonian. From the lower Turonian
Eck cites the following cephalopods :
Neolobites Schweinfurthi Eck
Fagesia bomba Eck
Fagesia cfr. tevesthenensis Peron
Vascoceras cfr. amieirense Choffat
Vascoceras Kossmati Choffat
aEck, Turon in Aegypten. (On account of the war I have not been able to obtain
the later work of the author.)
196 University of Texas Bulletin
Vascoceras Durandi Thomas et Peron
Vascoceras barcoicense Choffat
Pseudotissotia segnis Solger
Pseudaspidoceras cfr. Footeanum Stoliczka
Hoplitoides sp. (?)
Hoplitoides cfr. mirabilis Pervinquiere ( ?)
Southern Sahara: In Africa there are other localities where fossils
indicating- the existence of the Salmurian in a facies similar to that of
Portugal, Tunis, Egypt, etc., have been found. Chudeau1 describes some
cephalopods from Damergou, a region which lies nearly exactly where
Longitude 9°E Greenwich crosses Latitude 15°N. This author cites from
that part:
Vascoceras Cauvini Chudeau
Acanthoceras Gadeni Chudeau
According to the author Vascoceras Caudini is similar to V. Durandi
Thomas et Peron.
Nigeria? Woods2 describes several cephalopods from northern Nigeria
which seem to belong to Turonian forms. The species described are the
following :
Vascoceras Nigeriense Woods (similar to V. Durandi Thomas et
Peron)
Vascoceras Gongilense Woods (similar to V. subconciliatum Chof-
fat)
Pseudaspidoceras sp. (similar to Ps. Footeanum Stoliczka)
Hoplitoides Nigeriensis Woods (similar to H. Munieri Pervinquiere)
Kamerun: One can not doubt that the above cited fauna represents the
Turonian and probably the Salmurian; therefore it is rather astonishing
that a similar fauna has not been discovered in Kamerun, where only the
Neoptychites of the Mungo remind us of Salmurian forms. Solger sup-
poses that the Turonian exists in that region, but Guillemain and Harbort3
maintain that the beds in all their extension belong to the Emscherian.
From what we have seen in the foregoing description we conceive the
idea that in northern and central Africa and in Portugal exists a facies
of special features representing the Salmurian. This facies is distin-
guished by the frequence of the genera: Vascoceras, Fagesia, Neopty-
chites, Pseudaspidoceras, and in second place Pseudotissotia, Thomasites
and Hoplitoides.
Chudeau, Ammonites du Damergou, p. 66.
2Woods, Cret. dep. northern Nigeria, pp. 281-286.
3Guillemain und Harbort. Profil der Kreidesch. a. Mungo, p. 431.
A New Ammonite Fauna of the Lower Turanian of Mexico 197
Syria and Palestine: Of this characteristic fauna nothing seems to be
known in other parts of the Mediterranean. In Syria and Palestine,
Turonian beds are scarcely known. Notling cites from there a cephalopod
similar to Prionotropis Woolgari, and Diener cites a Mammites nodosoides.
This does not prove that .the Salmurian in its north African facies does not
exist there, because only a few years ago we did not know any more about
the Turonian of Egypt, until Eck published his first lists of cephalopods.
Southern France: It seems that on the European border of the Med-
iterranean the north African facies of the Salmurian with its character-
istic fauna of cephalopods is yet unknown. In France the same horizon
has quite a different fauna. In Provence there are, according to Gros-
souvre,1 beds with: Mammites nodosoides, M. conciliatus and Pseudo-
tissotia Douvillei, but at least the first two of these species are nearly
universally distributed types. Pervinquiere adds to this list Fagesia
Boucheroni Coquand. In Aquitania the following cephalopods have been
found : Pseudaspidoceras salmuriense, Fagesia superstes ?, Fagesia Bou-
cheroni Coquand, Fagesia tevesthensis, and Neoptychites cephalotus.
Thus this fauna contains quite a good number of the Salmurian fauna of
the Mediterranean, although in the case of Fagesia and Neoptychites it
seems that only very rare specimens have b.een found.
Saxony and Bohemia: The fauna of tli- Salmurian in Saxony and
Bohemia contains a still smaller number of elements which might belong
to the Mediterranean facies. Fritsch- describes from there as Mammites
conciliatus Stoliczka a form which certainly belongs to this group, although
as Kossmat already has noted, the species is different. The same author
cites Acanthoceras Neptuni. Laube and Bruder3 figure Mammites nodo-
soides and other species of this genus, as well as Puzosia Austeni. Petra-
scheck* cites Mammites Footeanus Stoliczka, Mammites cfr. crassitesta
Stoliczka, Barroisiceras ( ?) Fleuriausianum d'Orbigny, Acanthoceras cfr.
Choffati Kossmat; all forms of groups which in part occur around the
Mediterranean and in part in India.
Northern Europe: The faunas of the Salmurian of northern France
and nothern Germany show much less similarity with the Mediterranean
facies. They contain only ammonites belonging to groups of a universal
distribution, like Mammites nodosoides, Barroisiceras (?) Fleuriausianum,
Acanthoceras Neptuni, Pachydiscus peramplus, Puzosia Austeni, etc. Of
course, we have to take into consideration that neither in northern Ger-
'Grossouvre, Craie Superteure, Stratigr., p. 507.
2Fritsch, Ceph. bohm. Kreideform., p. 35.
3Laube und Bruder, Amm. d. bohm. Kreide, p. 229.
«Petrascheck, Amm. d. sachs. Kreideform., p. 155.
198 University of Texas Bulletin
many nor in Bohemia is there a modern stratigraphic-paleontological work
on the Turonian fauna.
Less still do we know about England, from which Solgar could cite
only a very few species as probably of Turonian age.
From the foregoing we see that the more we advance toward the north,
the more the elements belonging to the Mediterranean facies of the Sal-
murian diminish.
India: Certain faunal relations exist between the Salmurian of India
and that of the Mediterranean. In India the group of Mammites nodo-
soides is represented by two species, Mammites conciliatus Stoliczka and
M. crassitesta Stoliczka; the group Pseudaspidoceras by one, Ps. Footea-
num Stoliczka. The genus Fagesia is represented by two species, Fagesia
superstes Kossmat, and F. Rudra Stoliczka. In the same manner we find
Neoptychites represented by two species: Neuptychites Telinga Stoliczka
(=cephalotus Courtiller according to Pervinquiere) and N. xetra Stoliczka.
Japan: In Japan there is probably also Turonian with elements of the
Mediterranean facies. Yabe cites the occurrence of beds with Mammites.
In these he found a Mammites of the group of M. nodosoides Schlotheim.1
The same author describes a Fagesia Kotoi which occurs either in the same
beds or in those with Scaphites, which are a little younger.
Australia: It seems that in Australia the Turonian has not yet been
found; at least the fossils found in the Desert Sandstone, considered by
Jack and Etheridge as the representative of the upper Cretaceous,2 do not
allow such a conclusion.
Brazil: In South America only very few localities have been discov-
ered where fossils of the Salmurian have been found. Some species were
described from Brazil by White but without any indication of their age.
Several authors have already noted that the Salmurian must exist there,
but it seems nearly impossible to separate the Salmurian fossils from
those of the other Cretaceous horizons. Pervinquiere notes the similarity
between Vascoceras Durandi and Ammonites Harttii Hyatt,3 while Choffat
who had before that time called attention to the similarity between that
species and his Vascoceras harttiforme Kossmat believes that A. Harttii
might be a Fagesia, but the suture published by Hyatt4 shows that the
species belongs to Vascoceras.
Kossmat has also indicated the similarity between Ammonites pedroanus
iYabe, Strat. u. Pal. Hokkaido, p. 441.
-Jack and Etheridge, Queensland, p. 557 et seq.
3White, Brazil, p. 226, pi. 19, figs. 1, 2; pi. 20, fig. 3 (erroneously called A. Pedroanus
in the explanation of the plate and in the text).
*Hyatt, Pseudocer., pi. 14, fig. 16.
A New Ammonite Fauna of the Lower Turanian of Mexico 199
White1 and Pseudaspidoceras Footeanum Stoliczka. This species is found
at the same locality (Bom Jesus, Larangeiras, Provincia de Sergipe) where
Vascoceras Harttii occurs. It is therefore probably safe to say that the
Salmurian exists in that region in a facies similar to that of northern
Africa.
Pervinquiere finally has noted that his Vascoceras polymorphism is very
similar to Ammonites offarcinatus White,2 a species found at Trapiche
das Pedras Velho, Porto dos Barcos and Bom Jardin in the Province of
Sergipe. It seems to me probable that this type belongs to the multi-
tuberculated Vascoceras.
Peru: Species from the Salmurian have also been found in Peru. Lis-
son3 described and figured in 1908 two specimens of Vascoceras which he
identifies with Vase, amieirense Choffat. There can be no doubt that this
form is a real Vascoceras very similar to Vase, amieirense, although the
Peruvian form is a little more involute and the cross-section different.
Later on Lisson4 cites from Cuesta de Huanambra, in the province of Caja-
marca, a Mammites nodosoides var. Afra Pervinquiere, but notes that the
fossil seems to occur in the lower Senonian (Emscherian). From the
same locality he cites Hoplitoides ingens v. Koenen ; this makes the deter-
mination of the first species doubtful or indicates that both the Salmurian
and the Emscherian exist in this locality. This latter opinion is con-
firmed by a geological cross-section published by Schlagintweit,5 whose
locality "Cuesta de Huanyanba," is probably identical with the "Cuesta de
Huanambra" of Lisson, as both indicate that the place lies to the west of
Celendin. Schlagintweit gives the following cross-section:
6. Senonian beds.
5. Few meters of marly limestones of yellow color with Mammites
nodosoides Schlotheim. Turonian.
4. About 15 m. sandy dolomitic limestone.
3. Few meters of yellow marls of the Cenomanian with Exogyra
columba Lamarck.
2. 100-150 meters of light-colored limestone. Vraconian.
1. Aptian-Gault with fossils.
United States: In the rest of America no fauna similar to the Medit-
erranean facies of the Salmurian appears to have been discovered. In the
western United States the Turonian is represented by the Eagleford shales,
'White, Brazil, p. 213, pi. 22, figs. 1, 2 (won pi. 20, fig. 3).
'White, Brazil, p. 219, pi. 23, figs. 3, 4.
sLisson, Amm. del Peru, p. 9, 9a, 9b.
4Lisson, Terr, recon. en el Peru, II, p. 1.
5Schlagintweit, Vravon u. Cenoman i. Peru, p. 57.
200 University of Texas Bulletin
similar to the beds of Mexico, with Inoceramus labiatus ; and in the central
United States by the Benton and the Colorado formation. This latter
probably contains also the Emscherian. The cephalopods collected in these
beds are entirely different from those of the Mediterranean Salmurian
and seem to occur in slightly younger beds. Possibly the Salmurian may
yet be found in Texas, as there is only a short distance between this state
and our locality.
From the foregoing we reach the conclusion that our fauna of Cerro
del Macho has very near relations with the African and Portuguese facies
of the Salmurian and that a similar fauna probably exists in South Amer-
ica on the Pacific coast (Peru) as well as on the Atlantic border (Brazil).
In South America, especially in Peru, the similarity with the faunas of
north Africa appears to begin even in the Cenomanian (Schlagintweit)
and to persist still in the Senonian (Lisson), while in Mexico we can
not say the same, although in the Cenomanian as well as in the Senonian
there exist certain elements which remind us of forms from north Africa.
We certainly have to take into consideration that the fauna of the Ceno-
manian of Mexico is still very little known, only the faunas of Cerro del
Muleros and of the Vraconian of Camacho, Zacatecas, having been studied
in detail; and this latter fauna resembles entirely that of Europe. The
few fossils contained in the probably Cenomanian beds of Cerro del Macho
seem to indicate in a certain degree that the upper Cenomanian of this
region has a fauna similar to that of north Africa; but this problem
can only be solved in the future when larger collections have been made.
The Salmurian faunas of the African-Portuguese region as well as those
of Cerro del Macho have some, although not very near, relations with the
Salmurian of India and Japan, the connecting elements consisting of a few
groups of Mammites, Pseudaspidoceras, Fagesia and Neoptychites; and
we might even say that our facies is as much related to that of India and
Japan, as it is to that of France and Saxony-Bohemia.
I do not pretend that these results are to be considered as definite,
because the Salmurian in general is yet very little studied, not only in
far away countries like India and Japan but also in a great part of Europe.
PALEONTOLOGY— CEPHALOPODA
METOECOCERAS Hyatt
Hyatt1 proposed the name of Metoecoceras2 for the forms belonging to
the group of Ammonites Swallovi Shumard and united in the genus the
iHyatt, Pseudocer., p. 116.
2I accept the proposal of Pervinquiere to change the original name Metmcoccras
into Metoecoceras.
A New Ammonite Fauna of the Lower Turanian of Mexico 201
following species : M. Swallowi Shumard, M . gibbosum Hyatt, M. Whitei
Hyatt, M. acceleratum Hyatt, and M. Kanabense Hyatt (figured but not de-
scribed). These are forms similar to Acanthoceras in one direction and to
Pulchellia in the other ; they are always involute, with relatively flat flanks,
a nearly rectangular or lanceolate cross section, much higher than broad.
The ornamentation consists of straight or slightly flexous ribs which begin
at the umbilical border without forming real nodules in that region, al-
though in some cases they show slight thickening in that place. The ribs
continue on the flanks, showing near the ventral border a thickening or
very little pronounced nodule, and on the ventral shoulder a very sharp nod-
ule which is somewhat longitudinally prolonged and very near the above
mentioned thickening. Between the main ribs other secondary ribs are
intercalated which begin above the umbilical border in different heights ;
the main ribs are often bifurcated. Between the two rows of nodules on
the ventral shoulders there is a flattened zone, smooth in some cases while
in others the very low ribs cross this zone. The nodules of the two ventral
shoulders frequently form a kind of undulated or interrupted keels.
The suture of small individuals resembles that of Heinzia and Pulchellia,
while that of larger specimens is similar to the suture of certain groups of
Acanthoceras (Mantelliceras) and Acompsoceras. Characteristic is the ex-
ternal saddle divided by a secondary rather deep lobe ; the first lateral lobe
is broad and not very deep, the first lateral saddle is narrow but in general
higher than the external saddle; the second lateral lobe is narrow and
short, showing scarcely half of the depth of the first one. The second lat-
eral saddle is similar to the first one but much lower; there are always
three or four auxiliary saddles or even more in very large specimens. All
the saddles are very little ramified, the auxiliary ones often entirely whole.
The first lateral lobe seems to be always bifid.
Very characteristic also is the manner of involution in this genus. While
the internal whorls are completely involute, the external whorl covering
the greater part of the inner one, we see that the larger whorls and the
animal chamber show a much wider curve and cover a much larger part of
the next smaller whorl.
The species belonging to this group are so characteristic that one has to
consider them as an independent genus or subgenus. Hyatt considers this
group as a special family, giving it a position between the Heinzidae and
the Mantelliceratidae.
To the species united by Hyatt in the genus Metoecoceras we probably
have to add some European forms. One of these is Pulchellia Gesliana
Petrascheck1 from the upper Cenomanian of Saxony. Petrascheck con-
1Petrascheck, Amm. d. sachs. Kreideform., p. 140, pi. 7, figs. 3-5.
202 University of Texas Bulletin
siders this species as a Pulchellia and it certainly has the greatest sim-
ilarity with this genus if we do not take into account Metoecoceras. . Com-
paring the figures of Petrascheck with those of the American Metoeco-
ceras we note a surprising similarity ; for example, between figure 4 of Pe-
trascheck and figure 2 of Stanton,1 and between, figure 3 of Petrascheck
and figure 10 of plate 15 of Hyatt.2
The suture of the specimens from Saxony is imperfectly known, but the
elements which can be recognized in figure 4 of plate 7 and figure 5 of the
text (p. 141) of Petrascheck, coincide very well with those of Metoecoceras.
Petrascheck identifies his specimens with Ammonites Geslianus d'Or-
bigny,* but Sayn points out that the figure of d'Orbigny differs very much
from the figures of Petrascheck. It is possible that Ammonites Geslianus
d'Orbigny belongs also to Metoecoceras but this can not be decided as long
as the suture is entirely unknown. The specimen figured by Gueranger"
under the name of A. Geslianus is so badly preserved that no details can be
recognized. What Geinitz5 figures as A. Geslianus d'Orbigny seems to
differ considerably from the type and belongs perhaps to Stoliczkaia. Pe-
trascheck accepts the determination of Geinitz but does not figure any
specimen which shows the transition between the smooth ventral part and
the form in which the ribs pass the venter without interruption.
Kossmat6 has noted the external similarity between Acanthoceras vici-
nale Stoliczka7 and "Buchiceras" Swallovi Shumard, indicating at the same
time the difference in the suture which is much more complicated, especially
in the auxiliary saddles of the Indian species.
Still more similar to M. Swallovi is a cephalopod from Madagascar de-
scribed by Boule, Lemoine and Thevenin8 under the name of Acanthoceras
(Prionotropis) subvicinale. The suture of these specimens coincides per-
fectly with that of Metoecoceras, as has already been observed by the au-
thors, but it also has a great similarity with Pulchellia. The specimens are
very small and show an ornamentation very similar to that of Metoecoce-
^tanton, Colorado Form., p. 168, pi. 38 (Buchiceras Swallovi White; according to
Hyatt, this is a new species, M. Whitei, Hyatt).
2Hyatt, Pseudocer. •
3D'Orbigny, Pal. fran c.,terr. cret., ceph. p. 325, pi. 97, figs. 1-2 (under the name of
Am. catillus Sow.; this determination was corrected by d'Orbigny in Prodrfime II,
p. 146).
4Gueranger, Album Paleontol., pi. 5, fig. 2.
5Geinitz, Elbthalgebirge I, p. 280, pi. 62, fig. 3.
6Kossmat, Siidind. Kreideform., p. 201 (105).
'Stoliczka, Ceph. Cret. Rocks India, p. 84, pi. 44. Kossmat, Siidind. Kreideform..
p. 200 (104), pi. 25 (11), fig. 2.
"Boule, Lemoine et Thevenin, Diego-Suarez, p. 31, pi. 8, fig. 5; fig. 16 of the text.
A New Ammonite Fauna of the Lower Turonian of Mexico 203
ras; they differ principally by the presence of a median row of scarcely
perceptible, very small tubercles on the ventral part. Unfortunately the
specimens are all very small, therefore we can not know if this row of tu-
bercles becomes stronger in larger specimens, or if it disappears com-
pletely, or if it persists in larger individuals in the same manner as in
juvenile specimens. Hyatt does not mention the existence of a median
row of tubercles in juvenile specimens of Metoecoceras. Acanthoceras
subvicinale occurs in the Cenomanian of Diego-Suarez.
Thus we see that in Europe as well as in India and Madagascar there
seem to exist forms which resemble the Metoecoceras of America. Prob-
ably we have to include in this genus at least Pulchellia Gesliana Petras-
check and perhaps also Ammonites Geslianus d'Orbigny. Very similar is
also Acanthoceras subvicinale Boule, Lemoine et Thevenin, especially on
account of the suture, while Acanthoceras vicinale Stoliczka, although
showing a very similar ornamentation, differs by its more complicated
suture. But we should note that the suture changes considerably in the
different Metoeceras of America, that of M. Whitei being much more com-
plicated than that of M. Swallovi (in the limitation of Hyatt). At pres-
ent we can not decide how many forms should/ be included in the genus
Metoecoceras, but can only indicate that this genus is probably represented
in the Cenomanian of Europe and perhaps of Madagascar, and that similar
forms but with a much more complicated suture, are found in the Ceno-
manian and Turonian of India.
METOECOCERAS aff. WHITEI Hyatt
»
PL 12 figures 4, 7
1876: Buchiceras svallovi White, Inv. foss. Nevada, Utah, etc., p. 202, pi. 20.
1893: Buchiecras svallovi Stanton, Colorado Form., p. 168, pi. 37, fig. 1 (?pl. 38,
figs. 1-3).
1903: Meloicoceras Whitei Hyatt, Pseudocer., p. 122, pi. 13, figs. 3-5, pi. 14, figs. 1-10,
fig. 15.
In the lower bed of Cerro del Macho occur two fragments of cephalopods
which greatly resemble the group of Metoecoceras Whitei: they are espec-
ially similar to specimens figured by Hyatt. Our individuals show the fol-
lowing features :
Shell discoidal, very involute, with whorls of nearly rectangular cross
section, much higher than broad. The flanks are very little convex, nearly
flat, the ventral portion is flattened. The umbilicus is extremely narrow.
The ornamentation consists of strong ribs which begin on the umbilical
204 University of Texas Bulletin
border; they are slightly thickened near the umbilical border but do not
form real nodules. Between these main ribs other secondary ones are in-
tercalated ; they begin above the umbilical border and are a little less strong
on the flanks than the main ribs. The ribs are slightly bent forward on
the flanks but do not considerably increase in strength. Near the ventral
shoulder the ribs show a tuberculiform thickening and from this point
bend more strongly forwards ; they end on the ventral shoulder in a strong
nodule which is longitudinally prolonged. Between the two rows of nod-
ules on the ventral shoulders we observe an entirely flat and smooth zone
of the venter ; the ribs do not continue over the ventral portion, but every
pair of the ventral nodules is connected by a slight thickening, which pro-
duces on the ventral zone a slight undulation.
The suture is only partly visible. We recognize the external saddle, the
first lateral lobe, the first lateral saddle and the second lateral lobe. The
suture is not very well preserved because this part of the specimen is some-
what corroded, but still we are able to note the general character. The ex-
ternal saddle (compare figure) is broad and divided into two parts by a
rather deep secondary lobe ; the first lateral lobe is broad and shallow, end-
ing in two points, and on the sides are two rather large branches ; the first
lateral saddle is higher than the external one, its ramifications are few and
simple ; the second lateral lobe is much shallower than the first one, and it
is also narrower and trifid. In this specimen the umbilical portion is not
preserved but one sees that the second lateral saddle remains rather far
from the umbilicus, therefore several auxiliary lobes and saddles must have
existed in the intermediate space.
Figure 1. Metoecoceras aff. whitei Hyatt, suture
The ornamentation of our specimens coincides perfectly with that of
Metoecoceras Whitei Hyatt, only on the ventral part we do not observe as
A New Ammonite Fauna of the Lower Turanian of Mexico 205
deep furrows as in Hyatt's plate 13, figure 3, but simply an undulation. As
far as the suture is visible it corresponds with that of M. Whitei, especially
with that of plate 14, figure 8 of Hyatt. I do not identify my specimens
with M. Whitei because they are not sufficiently well preserved, but I am
sure that they belong to the group of M. Whitei.
We know very little about the stratigraphic position of M. Whitei; some
of Hyatt's originals have been found in the Kanab Valley, Utah. According
to Walcott and Stanton1 the species occurs there up to a height of 335 feet
above the base of the Cretaceous. Stanton refers that division to his Colo-
rado Formation which probably contains several horizons, perhaps from
the upper Cenomanian, or at least from the lower Turonian to the Emsche-
rian. For the determination of the age of our beds the species found in the
United States do not help us much. On the other hand, we do not know any
European form which might be identified with our species, although this
has a great similarity with Pulchellia Gesliana Petrascheck from the upper
Cenomanian of Saxony, as we have shown in the stratigraphical part.
Number of specimens : 2.
A//e: Upper Cenomanian (?), lower beds of Cerro del Macho.
METOECOCERAS sp. nov.
PI. 12, figs. 1-3
The collection of Dr. Haarmann contains a specimen of Metoecoceras
which is certainly different from the species described above ; unfortunately
we do not know in which horizon this specimen has been found ; according
to its petrographical character it belongs to Horizon I, but it might have
been found also in Horizon II. Its features are :
Shell discoidal, very involute, with whorls of a lanceolate cross section
truncated in the ventral part, much higher than broad. The flanks are a
little convex, the ventral' portion is flattened. The ornamentation consists
of rather strong ribs, which are slightly flexuous and which bend forward.
These begin near the umbilical border, where they are slightly thickened,
but do not form nodules. Part of these ribs bifurcate below the middle of
the height of the flank. Between these main ribs we find other secondary
ones intercalated which begin in different heights of the flank, and which at
their beginning are less strong than the main ribs. All the ribs show near
the ventral shoulder a slight thickening of a kind of very low and rounded
nodules ; on the ventral shoulder the ribs end in a nodule which is longi-
tudanally elongated. These nodules form together a kind of interrupted
'Stanton, Colorado Form., p. 35.
206 University of Texas Bulletin
keel on both sides of the ventral portion. Between the rows of nodules we
observe on the ventral portion a rather broad, flat and smooth zone.
With respect to the involution we observe that the last whorl seems to
show a tendency to form a wider curve than the preceding whorl.
No part of our specimen shows a trace of the suture.
According to its form and ornamentation our specimen belongs certainly
to Metoecoceras, and I unite it provisionally with this genus although the
suture is unknown.
The species differs from M. Whitei Hyatt typus in its' flexuous ribs, but
it resembles the specimens figured by Stanton1 in figures 1-2 of plates 38 and
called Buchiceras Swallovi. Hyatt unites it with his Metoecoceras Whitei,
notwithstanding that it differs much from the type. It seems that our spec-
imen has a smaller number of ribs than that figured by Stanton and that the
ribs are more flexuous.
Our species resembles much more Pulchellia Gesliniana Petrascheck2 than
the above described species. This similarity is really very great but our
species is distinguished by a smaller number of ribs which are also less
flexuous. I do not doubt that both species belong to the same group. Meto-
ecoceras Geslinianum Petrascheck occurs in the upper Cenomanian in
Saxony.
Number of specimens : 1.
Age : Upper Cenomanian ( ?) or lower Turonian.
MAMMITES Laube et Bruder, Emend. Petrascheck
MAMMITES MOHOVANENSIS sp. nov.
PI. 12, figs. 6, 8
In Horizon II of Cerro del Macho there has been found a well preserved
specimen of Mammites, and also several fragments belonging to the same
species. They show the following features :
Shell globose, rather involute, with whorls of a trapezoidal or nearly
subquadrangular cross section, much broader than high. The umbilicus is
rounded. On the umbilical border we observe six thick nodules, which are
rather pointed and a little rounded. In these nodules begin broad, rounded,
radial ribs, partly simple, partly in pairs. Between these ribs are interca-
lated generally two secondary ribs also low and rounded, which begin above
the umbilical border, but without showing nodules at their beginning. On
these secondary, as well as on the main, ribs we find two strong and rounded
1Stanton, Colorado Form.
2Petrascheck, Amm. d. sachs. Kreideform., p. 140 (10), pi. 7 (1), figs. 3-5.
A New Ammonite Fauna of the Lower Turanian of Mexico 207
nodules near and on the ventral part. These nodules form two rows, each
of which is composed of 16 to 17 nodules on the last whorl ; those of the row
on the ventral portion are a little elongated longitudinally. Thus we find
on each side of the shell three rows of nodules : the umbilical, the interme-
diate and the ventral row. It seems that the nodules of the intermediate
row increase in thickness in the front part of the whorl, while those of the
ventral row decrease a little and extend themselves more longitudinally,
but none of the specimens is large enough to show the development of the
nodules in an advanced age. Between the two ventral rows we observe a
narrow concave zone in the inner whorl and a nearly flat one on the exter-
nal whorl.
The suture is very much destroyed but its main features can still be
recognized. The external lobe is rather deep and narrow, ending in two
branches ; the external saddle is broad and high, divided into two branches
by an adventive lobe of relatively great depth ; the first lateral lobe is deep
and ends in two points ; the first lateral saddle is apparently broad but its
exact form can not be recognized because the shell is much destroyed in
this part.
Dimensions:
Diameter 87.0 mm. (1)
Height of the last whorl 33.0 mm. 0.38
Width of the last whorl 42.0 mm. 0.48
Diameter of the umbilicus 23.0 mm. 0.26
Height of the last whorl in the same diameter but half a whorl
backwards 30.5 mm. 0.35
Width of the last whorl in the same diameter and half a whorl back-
wards 39.0 mm. 0.46
Our species certainly belongs to the group of Mammites nodosoides
Schlotheim. Its suture coincides in general fairly well with the one figured
by Laube and Bruder1, but its form and ornamentation resemble more that
of Mammites conciliatus Stoliczka,2 which differs from the type of the group
especially by the greater thickness of the whorl and the more numerous
nodules on the ventral portion.
Our species differs from Mammites conciliates by its more involute
form, the external whorl covering nearly two-thirds of the preceding one.
barely leaving uncovered the row of umbilical tubercles. We find another
difference in the number of intermediate and ventral nodules, which is
much less in our specimen than in the species of Stoliczka. In this direc-
tion our individuals resemble more the type of Mammites nodosoides, but
'Laube und Bruder. Amm. d. bohm. Kreide, p. 230.
2Stoliczka, Ceph. Cret. Rocks India, p. 99. pi. 50, fig. 4; pi. 51, fig. 1.
208 University of Texas Bulletin
they differ from this as well as from M. conciliatus through the small dis-
tance between the two ventral rows of nodules. In these comparisons I
take as type of the species M. nodosoides, the specimen figured by Laube
and Bruder because this comes from the same locality as the originals of
Schlotheim, which were never figured.
Similar to our specimens is also the small individual figured by Pervin-
quiere1 as a typical M. nodosoides.
Fritsch2 figures a Mammites under the name of Ammonites conciliate
Stoliczka, and Kossmat3 confirms the conclusion that this specimen is very
nearly related to the species from southern India; he notes that the main
difference consists in the involution. In this direction the Mammites con-
ciliatus Fritsch resembles more our species than that of Stoliczka. Though
in this latter species the external whorl barely covers the preceding one up
to the row of intermediate nodules, we observe that in the specimen fig-
ured by Fritsch the external whorl covers the preceding one nearly to the
row of umbilical nodules.
The group of Mammites nodosoides has a quite universal distribution ;
it is represented in the lower Turonian of all Europe, of Africa, Asia, and
South America. In North America we probably find it represented by
Ammonites Loewianus White,4 an observation previously made by Per-
vinquiere.
Number of specimens: 3.
Age: Lower Turonian (Salmurian), lower horizon.
PSEUDASPIDOCERAS Hyatt emend. Pervinquiere
PSEUDASPIDOCERAS aff. FOOTEANUM Petrascheck
1902: Mammites Footeanus Stoliczka, Petrascheck, Amm. d. sachs. Kreideform., p. 144,
pi. 9, fig. 1.
Among the material collected by Dr. Haarmann in the lower horizon of
the Turonian of Cerro del Macho is a rather large, not very well preserved
but quite characteristic cephalopod, showing the following features :
Shell moderately evolute with whorls of a subrectangular-oval cross-
section, much higher than broad. The flanks are flattened, the ventral
portion rounded. The umbilicus is moderately wide, the umbilical wall is
1Pervinquiere, Paleontologie Tunisienne, pi. 18, fig. 1.
2Fritsch, Ceph. bohm. Kreideform., pi. 7, figs. 1, 2.
'Kossmat, Siidind. Kreideform., p. 22 (129).
4Stanton, Colorado Form., p. 178, pi. 43. figs. 3-4. Some authors write Am laevi-
anus but it must be Loewianus because the species was dedicated to Dr. Oscar Loew.
A New Ammonite Fauna of the Lower Turanian of Mexico 209
abrupt. The ornamentation consists in widely separated, low, rounded,
nearly straight ribs which begin in a nodule at the umbilical border and
which end in another very high and pointed nodule at the ventral shoulder.
Between the two rows of nodules on the ventral part we observe a broad,
slightly convex and smooth zone. In the last half whorl we count five ribs.
The suture is not visible.
Dimensions:
Diameter 280mm. (1)
Height of the last whorl 117 mm. 0.42
Width of the last whorl 94 mm. 0.34
Diameter of the umbilicus 104 mm. 0.37
Our specimen certainly belongs to the group of Pseudaspidoceras Foot-
eanum Stoliczka,2 but differs from it by its cross-section which is much
higher than wide. This is not an absolutely distinctive character because
we should take into consideration the large size of our specimen and we
do not know the latest development of the species of Stoliczka. Our speci-
men resembles Pseudaspidoceras Footeanum Petrascheck more than it
does the type. The cross-section of the species of Petrascheck is more
similar to ours and also has widely separated ribs.
The group of Pseudaspidoceras Footeanum Stoliczka has a very wide
distribution; it is represented in all the northern part of Africa (we in-
clude in this group Ps. salmuriense) , in Nigeria, in Portugal, in Saxony,
and in India.
Number of specimens : 1.
Age: Lower Turonian (Salmurian), lower horizon.
PSEUDASPIDOCERAS aff. PEDROANUM Whit^
PL 13, fig. 1; PL 15, fig. 1
1887: Ammonites Pedroanus White, Brazil, p. 212, pi. 22, figs. 1, 2 (not pi. 20, fig. 3).
In the lower horizon of the Turonian of Cerro del Macho we find a large
and relatively well preserved specimen which belongs to the group of
Pseudaspidoceras Footeanum Stoliczka. Its features are:
Shell large with whorls of a subquadranglar cross-section, nearly as
high as wide. The flanks are flattened, the ventral portion is nearly flat.
The umbilicus is relatively wide and deep, the umbilical wall is vertical
but without a sharp umbilical shoulder. The external whorl covers only
the ventral portion of the preceding one and leaves the nodules of the ven-
tral shoulder free. The ornamentation consists of extremely low and
2Stoliczka, Ceph. Cret. Rocks India, p. 101, pi. 52, figs. 1, 2.
210 University of Texas Bulletin
rounded, nearly straight ribs which sometimes are scarcely perceptible;
on the last whorl we count thirteen of these ribs. The ribs begin on the
umbilical border in a strong and pointed nodule and end with another
and still more prominent but somewhat longitudinally elongated nodule
on the ventral shoulder. Between the two rows on the ventral shoulders
we observe a smooth and very slightly convex zone which does not show
any signs of nodules or ribs ; only the two last nodules seem to be connected
by a kind of low rounded rib which crosses the smooth zone of the venter.
Between the nodules of the rows on the ventral shoulder we find some
ribs or nodules intercalated which do not correspond to umbilical nodules.
Traces of the suture are visible in different parts but I have not been
able to draw a complete line.
Dimensions :
Diameter: 214 mm.
The last part of our specimen bemg somewhat crushed and twisted, we
have taken the following dimensions frcm a little smaller diameter :
Diameter 164mm. (1)
Height of the last whorl 63 mm. 0.38
Width of the last whorl 70 mm. 0.43
Diameter of the umbilicus 59 mm. 0.36
Height of the last whorl on the same diameter but half a whorl back-
wards 42 mm. 0.26
Width of the last whorl on the same point 45 mm. 0.27
Our specimen belongs, as we have already mentioned, to the group of
Pseudaspidoceras Footeanum Stoliczka1 which it resembles in its involu-
tion, the cross-section of the whorls, the two series of prominent nodules,
etc. It differs from the type through its weaker ribs, and the entire ab-
sence of ribs and nodules on the ventral portion and of a concave zone
along the line of symmetry on the ventral portion.
Our species shows much nearer relations to Pseudaspidoceras pedroanum
White from Brazil than to the type of the group. It has the same kind of
involution, a very similar cross-section, a nearly identical ornamentation;
it only seems to differ a little with respect to the nodules on the ventral
shoulder, which according to the figure of White are connected on the
last part of the whorl by a kind of low crest, which is also mentioned in
the text. White also says that in very large individuals the nodules on
both sides of the venter are connected by a crest which crosses the venter.
We have indicated a similar phenomenon in the last two nodules of our
specimen. We thus see that our species resembles in a surprising man-
ner Ammonites pedroanus Kossmat and others have already recognized
A New Ammonite Fauna of the Lower Turanian of Mexico 211
that this species belongs to the group of Pseudaspidoceras Footeanum.
White compares his species with Ammonites Leonensis Conrad, which is
probably a Schloenbachia, and also with Prionotropis Woolgari.
We know nothing about the age of the beds where the type of the species
has been found but the similarity with Pseudaspidoceras Footeanum allows
us to conclude that they probably belong to the Salmurian. In this idea
we are confirmed by the circumstance that in the same locality Vascoceras
Harttii Hyatt has been discovered.
Number of specimens : 1.
Age: Lower Turonian (Salmurian), lower horizon.
FACES I A Pervinquie're
FACES I A HAARMANNI sp. nov.
PL 14, figs. 1, 2; PL 15, fig. 2
In the lower bed of the Salmurian of Cerro del Macho Dr. Haarmann
found a not quite complete specimen of so characteristic a Fagesia that I
have no hesitation in giving it a new name. Another more complete but
somewhat deformed specimen collected by Dr. E. Wittich, was given to me
by Mr. Federico Ritter. The features of the larger specimen are :
Shell moderately involute with whorls of transversally elliptical cross-
section, much broader than high. The umbilicus is rather narrow and
deep; the umbilical wall is abrupt, in the internal whorls nearly vertical.
The ventral portion is broad and slightly convex, the region of the flanks
is very narrow and one might say scarcely developed and in reality only
represented by the umbilical nodules ; the ventral part nearly touches the
umbilical wall. The ornamentation consists on the umbilical border of
some nine very strong, pointed and round nodules. From these nodules
start rounded, broad, rather high ribs which cross the ventral portion
without interruption in a curve directed toward the front; in general
a pair of ribs starts from each nodule and one or two more become inter-
calated between every two pairs. This disposition can not be observed
with entire certainty because the border of the whorl is a little broken.
The suture could not be made visible.
Dimensions:
Diameter 165 mm. (1)
Height of the last whorl 52 mm. 0.32
Width of the last whorl ?74 mm. 0.45
Diameter of the umbilicus 66 mm. 0.40
212 University of Texas Bulletin
At the first view1 our species resembles greatly a Stephanoceras, a simi-
larity which has been noted also in other species of Fagesia especially
Fagesia superstes Kossmat.1 From this species, which represents the type
of the genus, our species differs by being much more evolute and by its
stronger ribs; the umbilical nodules are less numerous and thicker, the
ribs are also less numerous and a little stronger.
Our species is certainly the most evolute one of all the Fagesia so far
described, but its nearest relative is without doubt Fagesia superstes
Kossmat. According to the figure published by Kossmat no nodules can
be seen on the internal whorls, while in our species these nodules can be
distinguished even on the smallest whorls.
The occurrence of this species is of certain stratigraphical importance
in so far as it belongs to a very characteristic group which seems at present
to be limited to the Turonian. According to Pervinquiere only six species
are known and all of these belong to the Turonian. Fagesia superstes,
which resembles ours more than any other species, has been found in
India (upper Utatur group) and in Tunis (lower Turonian) ; similar forms
have been discovered in the Turonian of Portugal and France.2
Number of specimens : 2.
Age: Lower Turonian (Salmurian), lower horizon.
FAGESIA PERVINQUIERI sp. nov.
PI. 14, fig. 3
In the lower horizon of our Salmurian we find a relatively well preserved
specimen which belongs to Fagesia but differs essentially from the fore-
going species by its entirely different form and the weaker ornamentation.
Its general features are:
Shell subglobose, very involute, with whorls of transversally semilunar
cross-section. The umbilicus is narrow and deep, the umbilical wall is
nearly vertical. On the umbilical border of the internal whorls appear
not very strong nodules; on the last part of the external whorl the um-
bilical border seems to be entirely smooth. On the internal whorl we
observe numerous broad and low ribs which are strongest in the central
part of the ventral portion, while they seem to flatten out toward the
umbilical border. On the ventral portion the ribs curve slightly toward
the front. The number of ribs could not be counted because the ventral
iRossmat, Siidind. Kreideform., p. 26 (133), pi. 6 (17), fig. 1.
2Pervinquiere, Paleontologie Tunisienne, p. 325, note 5.
A New Ammonite Fauna of the Lower Turanian of Mexico
portion of the last whorl is a little corroded, but there are certainly more
than forty on the last whorl. The suture is not visible.
Dimensions:
Diameter 94mm. (1)
Height of the last whorl 36 mm. 0.40
Width of the last whorl 60 mm. .0.64
Diameter of the umbilicus 31 mm. 0.33
Height of the last whorl on the same diameter but half a whorl
backwards 27 mm. 0.29
Width of the last whorl at the same point 55 mm. 0.59
On account of its general form and its ornamentation I place this speci-
men in the genus Fagesia although the suture could not be made visible.
Our species is quite similar to Fagesia tevesthensis Peron1 especially the
large specimen figured by Pervinquiere- (pi. 20, fig. 6). This individual
shows on the umbilical border nodules quite similar to those of our speci-
men. But the African species has much broader and lower whorls which
in part may be explained by its stage of development, because all the
species of Fagesia change their cross-section of the whorls with their age
and grow more rapidly in width than in height.
Another species which resembles ours is Fagesia rudra Stoliczka.3 This
species shows very similar ribs and the umbilical border is entirely smooth.
Fagesia rudra differs from our species by its much broader and lower
whorls.
Unfortunately only a single specimen of our species has been found.
It was impossible to study the internal whorls in their details and there-
fore we can not make more detailed comparisons with other species.
Number of specimens: 1.
Age: Lower Turonian (Salmurian), lower horizon.
VASCOCERAS Choffat
When Choffat4 established his new genus Vascoceras he subdivided it
into four groups: 1. mono-tuberculated forms with wide umbilicus;
2. subglobose forms with rounded umbilical border ; 3. globose forms with
angular or subangular umbilical border; 4. multi-tuberculated forms.
These groups could be called: 1. Group of Vascoceras Gamai; 2. Group
'Peron, Amm. du Cret. sup. de PAlgerie, p. 23, pi. 7, figs. 2, 3.
2Pervinquiere, Paleontologie Tunisienne, p. 325, pi. 20, figs. 5, 6.
3Stoliczka, Ceph. Cret. Rocks India, p. 122, pi. 60, fig. 1.
«Choffat, Especes nouv. ou peu conn., p. 51.
21-1 University of Texas Bulletin
of Vascoceras Douvillei; 3. Group of Vascoceras harttiiforme; 4. Group
of Vascoceras subconciliatum.
Pervinquiere1 unites the first two groups in one and distinguishes only
three subdivisions. This seems to me to be the best solution, as the divi-
sion of the first two groups appears to be rather artificial.
Among the material of Cerro del Macho we find forms representing the
three groups. To the first one (in the sense of Pervinquiere) belongs our
Vascoceras aff. Gamai Choffat and Vascoceras aff. adonense; to the second
one Vascoceras Angermanni sp. nov., and perhaps Vascoceras aff. arnesense
Choffat; to the third one Vascoceras mohovanense n. sp.
The genus Vascoceras so far has been found in Portugal, Spain, Algeria,
Tunis, Egypt, the Sahara, Nigeria, Brazil, Peru, and Mexico.
VASCOCERAS sp. nov. ex aff. V. ADONENSE Choffat
PL 14, fig. 4; PL 17, fig. 2
1886: Vascoceras adonense Choffat, Especes nouv. ou peu conn., p. 59, pi. 9, fig. 3;
pi. 21, fig. 12.
Our specimen shows the following features:
Internal mold rather large, a little oblique on account of deformation,
quite evolute, with whorls of a transversally semi-lunar cross-section,
much broader than high. The umbilicus is wide, the umbilical wall is
quite abrupt, the umbilical border is rounded and scarcely subangular. In
the external whorl no nodules exist on the umbilical border; the internal
whorls are not visible. The surface of the species is smooth, no orna-
mentation can be distinguished.
The suture is very simple ; it is not very well preserved but the general
features can be well distinguished. The external lobe is quite wide and
not very deep and ends in two branches; the external saddle is wide at
the base, becoming narrower upward, and is very little ramified; the
first lateral lobe is funnel shaped, very wide at the mouth ; the first lateral
saddle is similar to the external one but smaller and inclined toward the
umbilicus while the external one rather bends over toward the venter;
the second lateral lobe is funnel shaped, very wide at the mouth and much
shallower than the first one; the second lateral saddle (on the umbilical
border) is similar to the first one but smaller.
The dimensions could not be measured exactly on account of the de-
formation of the specimen.
Pervinquiere, Paleontologie Tunisienne, p. 331.
A New Ammonite Fauna, of the Lower Turanian of Mexico 215
With respect to its external form our species resembles Vascoceras
adonense Choffat, but this latter species shows nodules on its umbilical
border, while these are entirely missing in our specimen. This might be
explained by the stage of development, our individual being much larger
than that of Choffat, but our species is certainly much more evolute. A
Figure 2. Suture, Vascoceras angermanni n. sp. (above) and Vascoceras aff. adonense
Choffat (below).
fundamental difference can be found in the suture. In the type species
we find on the umbilical border the first lateral saddle, but we see that
in our specimen the second lateral saddle is in this place. In its general
character our suture is much more similar to that of Vascoceras Gamai.
Our species therefore has to be considered as a new form which in its
external figure resembles Vascoceras adonense while the suture places it
in the vicinity of Vascoceras Gamai. We can not give it a new name
because the specimen is too badly preserved.
Number of specimens: 1.
Age: Lower Turonian (Salmurian), lower horizon.
2T6 University of Texas Bulletin
VASCOCERAS aff. GAMAI Choffat
PI. 15, figs. 3-5
1886: Vascoceras Gamai Choffat, Especes nouv. ou peu conn., p. 54, pi. 7, figs. 1-4;
pi. 8, fig. 1; pi. 10, fig. 2; pi. 21, figs. 1-5.
In the collection made by Dr. Angermann I found a cepholopod which
probably represents a juvenile stage of some species belonging to the group
of Vascoceras Gamai. Judging from the petrographical aspect of the
specimen I suppose that it was found in the upper horizon of the Salmurian
of Cerro del Macho. Its features are :
Shell relatively small, quite involute with whorls of a subquadrangular
rounded cross-section, broader than high. The umbilicus is narrow and
probably deep, the umbilical wall is abrupt. The flanks are flattened, the
ventral part rounded. On the umbilical border we count seven thick,
round, and pointed nodules. From each of these starts either a pair of
ribs or a simple rib, which curves slightly forward and crosses without
interruption the ventral portion. Between these main ribs one or two
secondary ones are intercalated. These begin above the umbilical border,
but on the venter are as strong as the main ones. The ribs are thick,
broad, rounded, wider than the interstices by which they are separated.
On the ventral shoulders the ribs seem to have u tendency toward a slight
thickening but real nodules do not form there. On the anterior part of
the last whorl, and especially on the ventral region, the ribs seem to dis-
appear. This region is partially corroded but in a place which is well
preserved one notes clearly that the ribs are very low and scarcely per-
ceptible on the line of symmetry.
Figure 3. Suture, Vascoceras aff. gamai Choffat
The suture is very little ramified. The external lobe has two branches
and is quite deep and narrow; the external saddle is little ramified, broad
and rounded ; the first lateral lobe is less deep than the external one and
rather narrow. The first lateral saddle is little ramified and resembles in
its form the external one, but is narrower.
Our specimen resembles the juvenile form figured by Choffat in figure 4
A New Ammonite Fauna of the Lower Turonian of Mexico 217
of plate 7 ; unfortunately no figure of the form viewed from the side has
been published. The juvenile specimen of figure 3 of plate 7, the lateral
view of which is given in figure 2 of plate 10 of Choffat is also similar.
The main difference exists probably in the smaller number of umbilical
nodules in our specimen and in the narrower cross-section, although this
latter feature changes with the age.
In the juvenile specimens of Vascoceras Mundae the ribs are less numer-
ous and thicker.
Vascoceras Gamai Choffat occurs in Portugal mainly in the lower and
middle Turonian of Choffat, both of which according to my opinion belong
to the Salmurian.
Number of specimens: 1.
Age: Lower Turonian (Salmurian), probably from the upper horizon.
VASCOCERAS ANGERMANNI sp. nov.
PI. 16, figs. 1-4; PI. 17, fig. 1
In the collection of Dr. Angermann as well as in that of Dr. Haarmann
we find a globose cephalopod which at the first view resembles completely a
Nautilus. In the collection of Angermann there is a small, quite well
preserved specimen, and in Mr. Haarmann's collection a much larger one,
but the features of both are the same. There are also a number of frag-
ments which probably should be united with this singular species. Its
features are :
Shell large, globose, extremely involute, with whorls of semi-lunar cross-
section, much broader than high. The whorls cover the preceding ones
nearly entirely. The umbilicus is narrow and deep, the umbilical wall
abrupt, the umbilical border smooth and angular. The surface of the
shell is entirely smooth without any nodules or ribs.
The suture is not very well preserved but its general features can be
well recognized. The external lobe is quite deep and moderately wide,
ending in two branches. The external saddle is moderately broad, quite
high, very little ramified ; the first lateral lobe is little ramified, broad, ends
in two points and is deeper than the external one ; the first lateral saddle
is broad and rounded, less high than the external saddle. The second lat-
eral lobe is probably similar to the first but less deep ; it is not entirely pre-
served.
Dimensions of the smaller specimen :
218 University of Texas Bulletin
Dimensions:
Diameter 75 mm. (1)
Height of the last whorl 32 mm. 0.45
Width of the last whorl 69 mm. 0.92
Diameter of the umbilicus 14 mm. 0.19
Height of the last whorl on the same diameter but half a whorl back-
wards 27 ^..-n. 0.36
Width of the last whorl at the same point 62 mm. 0.83
Diameter of the largest specimen : 124 mm.
Our species resembles greatly Vascoceras Kossmati Choffat1; it is of
course evident that all the species belonging to this group must be very
similar, as none of them shows any ornamentation. The main difference
between our species and Vascoceras Kossmati consists in the different
curve of the cross section of the internal whorls, which is always of
greater radius. The suture is also different, the saddles of our species be-
ing relatively higher and the lobes deeper. One might add that our species
grows to a larger size than the Portuguese species.
Vascoceras Kossmati Choffat has been found in Choffat's middle Turon-
ian of Portugal, which, according to my opinion, belongs to the Salmurian.
In Egypt it occurs in the lower Turonian.2 Our larger specimens have
been found in the upper bed of the Salmurian of Cerro del Macho and the
specimen collected by Angermann belongs to the same horizon, judging
from its petrographical character.
Number of specimens : 3 and several fragments.
Age: Lower Turonian (Salmurian), upper horizon.
VASCOCERAS sp.
PI. 18, fig. 12
Dr. Haarmann found in the upper horizon of Cerro del Macho a cepha-
lopod, the generic determination of which remains somewhat in doubt be-
cause its suture can not be made visible. Mr. Frederico Ritter gave me
another and a little better preserved specimen which shows traces of the
suture. Their features are :
Shell subglobose of moderate size, very involute with whorls of semi-
lunar cross section, broader than high. Flanks and ventral portion round-
ed. The umbilicus is small and deep, the* umbilical wall is vertical and
even a little overhanging; the umbilical border is angular. The shell
1Choffat, Especes nouv. ou peu conn., p. 63, pi. 13, figs. 8, 9; pi. 14, figs. 1, 2;
pi. 21, figs. 26, 27.
2Eck, Turon in Aegypten, p. 384.
A New Ammonite Fauna of the Lower Turanian of Mexico 219
seems to be entirely smooth, no nodules can be observed on the umbilical
border. The suture is similar to that of the group of Vascoceras Kossmati
but it is not complete enough for a drawing.
Dimensions :
Diameter 106 mm. (1)
Height of the last whorl 43 mm. 0.41
Width of the last whorl 72 mm. 0.68
Diameter of the umbilicus 22 mm. 0.21
One of the specimens is a little obliquely deformed which makes the de-
termination still more difficult. The species resembles externally much
Ammonites arnesensis Choffat1, the generic position of which is equally
doubtful; it seems to me to belong to Vascoceras or to a new subgenous,
the suture being quite different from that of the type of the genus.
In one of our specimens the suture is not visible ; in the other one we see
parts of it which are similar to the elements of the suture of Vascoceras
Angermanni. Therefore I place our species provisionally in the genus
Vascoceras. Externally this species resembles somewhat Vascoceras Ar-
germanm but the umbilicus is wider, the general form less globose, and
the whorls are less broad in relation to their height.
Number of specimens: 2.
Age: Lower Turonian (Salmurian), upper horizon.
VASCOCERAS MOHOVANENSE sp. nov.
PI. 18, figs. 1-2
Dr. Haarmann collected in the upper bed of our Salmurian a juvenile
individual of a cephalopod which certainly represents a new species. Its
features are :
Shell small, subglobose, quite involute with whorls of trapezoidal cross
section, much broader than high. The flanks are somewhat flattened,
as is also the ventral part. This gives the cross-section its angular form.
The umbilicus is narrow and deep, the umbilical wall is abrupt, the um-
bilical border is angular. The ornamentation consists in the last whorl of
about eleven high and pointed nodules (nearly all broken in the present
specimen) on the umbilical border; from each of these generally starts a
pair of ribs. Between this pair of ribs now and then secondary ribs are
intercalated which begin above the umbilical border. The ribs are thick
'Choffat, Especes nouv. ou peu conn., p. 68, pi. 13, fig. 10 ; pi. 14, fig. 3, pi. 22, fig. 39.
220 University of Texas Bulletin
and high. They become a little lower on the venter but cross it without
interruption; no longitudnal furrow exists on the venter. On the ventral
shoulders the ribs thicken a little, forming on each shoulder a row of ra-
dially elongated nodules ; these are not very strong and rather low. These
nodules make the ventral shoulders appear angular and the ventral zone
more flattened than concave.
Figure 4. Sutures, Vascoceras mohovanense n. sp (above) and Mammites mohovan-
ensis n. sp. (below).
The suture is very simple. The external lobe is quite wide and deep,
and bifid ; the external saddle is broad, low, or a rounded form and a little
ramified ; the first lateral lobe is wide, approximately as deep as the exter-
nal lobe but much wider, and it ends in two points ; the first lateral saddle
is very low, rounded and broad and lies in the umbilical nodule; the form
of the second lateral lobe, which lies mostly on the umbilical wall, can not
be well distinguished.
Dimensions :
Diameter 56 mm. (1)
Height of the last whorl 21 mm. 0.38
Width of the last whorl 45 mm. 0.80 (with the nodule)
Diameter of the umbilicus 19 mm. 0.34
Height of the last whorl on the same diameter but
half a whorl backwards 16 mm. 0.29
Width of the last whorl at the same point 34 mm. 0.61
This very characteristic species certainly belongs to the group of Vasco-
ceras sub conciliation Choffat1, but it resembles Vascoceras polymorphum
1Choffat, Espfcces nouv. ou peu conn., p. 64, pi. 15, figs. 1-3; pi. 16, fig. 4; pi. 22,
figs. 28-31.
A New Ammonite Fauna of the Lower Turanian of Mexico 221
Pervinquiere1 more than it does the type. From both species it differs
through the absence of an intermediate row of nodules and consequently
through the different cross section of tne whorl. From Vascoceras subcon-
ciliatum our species is also distinguished by its very reduced and simple
suture. In this case it resembles much more Vascoceras polymorphum
Pervinquiere, which shows a very similar suture.
Pervinquiere has extensively discussed the relations of Vascoceras poty-
morphum with the other Vascoceras, as well as with Mammites and Acon-
thoceras, indicating the similarity of certain groups of Aconthoceras and
Mammites, and emphasizing the singular nature of the suture, which is
similar to that of other Vascoceras. I believe that Pervinquiere's reasons
are well founded and that the present group should be placed in the genus
Vascoceras, especially as this genus is nearly related to Acanthoceras and
Mammites; therefore the similarity between certain groups of the three
genera is not very surprising.
Vascoceras polymorphum Pervinquiere occurs in the lower Turonian of
Tunis; Vascoceras subconciliatum Choffat is found in beds of a similar
age in Portugal. Pervinquiere also emphasizes the similarity between this
group and a cephalopod from Brazil, Ammonites offaccinatus White,2 but
this latter species is too little known to allow a detailed comparison. The
suture is not figured but according to White it is rather complicated. It
is therefore possible that it belongs to a different group, or even to a dif-
ferent genus.
Number of specimens : 1.
Age: Lower Turonian (Salmurian), lower horizon.
NEOPTYCHITES Kossmat
NEOPTYCHITES aff. CEPHALOTUS Courtiller
PI. 18, figs. 3, 10, 13
1907: Neoptychites cephalotus Courtiller Pervinqutere, Paleontologie Tunisienne, p. 393,
pi. 27, figs. 1-3. Cum syn.
•
Among our material exists a cephalopod of small size which in its ex-
ternal form and its suture resembles the juvenile specimens of Neoptychi-
tes. Its features are :
Shell subglobose, very involute, last whorl broader than high with nearly
Pervinquiere, Paleontologie Tunisienne, p. 336, pi. 21, figs. 2-5.
'White, Brazil, p. 219, pi. 23, figs. 3, 4.
222 University of Texas Bulletin
semilunar cross-section. The umbilicus is very narrow; the wall can not
be seen. The flanks are slightly convex, the venter is rounded. The orna-
mentation consists of low, rounded, broad, numerous ribs (about 32 to the
whorl) which apparently do not reach down to the umbilical region and
which are strongest on the ventral portion. On the internal whorl we note
a well defined and rather broad constriction which toward the front is
limited by a slight thickening ; the constriction is especially evident on the
venter. The ribs are curved forwards, as is the case with the constriction,
although in less degree.
Figure 5. Suture, Neoptychites aff. cephalotus Courtiller
The suture is very similar to that of Neoptychites and corresponds in
general to that of Neopychites cephalotus, although the figure published by
Pervinquiere is taken from a much larger specimen ; a little more similar
still is the suture of the small specimen of N. xetriformis, in the above cited
work of Pervinquiere (p. 398, fig. 153) , although there the external saddle
is more slender than in our specimen. The suture of our individual is not
complete and in some places can not be very well followed, but in general
narrow, ending in two branches; the external saddle is quite broad and
one recognizes the main features. The external lobe is deep and relatively
high and little ramified ; the first lateral lobe is a little shallower than the
external one, ends in two points and shows also a branch directed obliquely
toward the ventral region ; the first lateral saddle is similar to the external
one but is lower and narrower.
Figure 6. Suture, Neoptychites aff. cephalotus Courtiller
Dimensions :
Diameter ............................................. ...... 50mm. (1)
Height of the last whorl ............................ ^ ........ 2<5 mm. 0.52
Width of the last whorl ...... .......................... " . . ...... 33 mm. 0.66
Our specimen represents the juvenile stage of a Neoptychites similar to
the one figured by Pervinquiere in pi. 27 fig. 2, which it resembles much in
its external features ; it differs mainly in its great width. But according to
Pervinquiere the dimensions change much in the genus, and we should not
give too much importance to this feature. A specific determination of our
A New Ammonite Fauna of the Lower Turanian of Mexico 223
specimen is not possible on account of its small size ; we can only say that
it is a Neoptychites similar to Neoptychites cephalotits but probably a dif-
ferent species.
Neoptychites cephalotus occurs in the lower Turonian of Tunis, Altrerla
and France. Grossouvre proposes to unite it with Neoptychites Telinga.
Stoliczka and Pervinquiere accepts this opinion. There is no doubt that
the adult individuals of the two species resemble each other very much,
although the suture seems to be somewhat different and a little more rami-
fied in N. cephalotus; but this last character is not decisive as long as we
know only the suture of a very large specimen of N. Telinga.. A definite
result can only be reached through the study of the development of N. Te-
linga or at least of that of small specimens.
Number of specimens : 1.
Age: Lower Turonian (Salmurian), upper horizon.
NEOPTYCHITES aflf. XETRIFORMIS Pervinquiere
PL 18, figs. 9, 11
1907: Neoptychite xetriformis Pervinquiere, Paleontologie Tunisienne, p. 398, pi. 27,
figs. 5-7.
Among the material collected by Dr. Angermann is a very typical Neop-
tychites. The specimen is sufficiently well preserved for a generic deter-
mination. Its features are :
Shell discoidal, very involute, with whorls of nearly sagittiform cross
section, much higher than broad. The greatest width is near the umbilical
border. The flanks are quite flattened and very little convex, and the ven-
ter is rounded. The umbilicus is extremely narrow and deep ; the umbil-
ical wall is vertical ; apparently a slight thickening exists on the umbilical
border, at least in the last part of the external whorl. On the flanks we
observe radial, broad, low, and rounded ribs which are strongest in the
region near the venter and which decrease in strength toward the umbilical
as well as toward the ventral region ; they disappear near the umbilicus.
On the venter the ribs are very low and scarcely discernible ; near the ven-
tral portion, they bend forward. The number of ribs could not be counted
because part of the surface is corroded.
The suture is not very well preserved but the main features can be rec-
ognized. The external lobe is relatively wide and shallow, ending in two
short branches; the external saddle is not very high nor very broad but
little ramified. The first lateral lobe is wide and ends in two points ; it also
has a branch on each side, and is deeper than the external lobe. The first
224 University of Texas Bulletin
lateral saddle is narrow, a little lower than the external saddle, and little
ramified ; second lateral lobe is similar to the first in its form but smaller
and much shallower ; the second lateral saddle is very low and very broad
and of oblique form.
Dimensions :
Diameter 73 mm. (1)
Height of the last whorl 40 mm. 0.55
Width of the last whorl 33 mm. 0.45
Diameter of the umbilicus 6.5 mm. 0.09
With respect to its external form our specimen is very similar to Neop-
tychites xetriformis; even the dimensions coincide sufficiently, if we take
into consideration the variability of Neoptychites. The main difference
consists in the ornamentation; the ribs are much more numerous in our
species (probably 25 to 30 on the last whorl) and they do not disappear
completely on the venter. The specimen thus occupies an intermediate
position between N. cephalotus and N. xetriformis, or between this and
2V. xetra, if the small individual figured by Stoliczka1 really belongs to N.
Xetra. The suture of our specimen resembles that of N. Xetra still more
than that of N. xetriformis.
N. xetriformis occurs in the lower Turonian of Tunis. N. Xetra
Stoliczka belongs to the lower and middle Utatur group according to Koss-
mat, but we should not forget that the determination of the horizons of
the Utatur group is in general based on the petrographical character of
the fossils and on the locality. The determination of the age is therefore
not always certain for each species. How doubtful it sometimes is we can
see in our own case. On page 168 (72) Kossmat cites N. Xetra from the
lower and middle Utatur group; on page 196 (131) he cites it from the
lower and upper Utatur group. This doubt with respect to the age of the
different species can not surprise us. because Kossmat could not base his
determinations on well divided and stratigraphically well studied cross
sections, but rather on general observations and subdivisions based more
on the petrographical character of the rocks than on the faunas. Kossmat
himself (loc. cit. p. 132 (197)) is convinced that a paleontological and
stratijrraphical subdivision of the Utatur group is possible, but until this
has been executed in a modern manner, we should not crive too much im-
portance to the age which has been assigned to a certain species from In-
dia. We should always take into account that in such old collections labels
'Stoliczka, Ceph. Cret. Rocks India, pi. 61, fig. 2.
A New Ammonite Fauna of the Lower Turanian of Mexico 225
may have been changed and that the fossils frequently have not been col-
lected with the necessary exactness.
Number of specimens : 1.
Age: Lower Turonian (Salmurian), lower horizon.
HOPLITOIDES V. Koenen Emend. Solger et Pervinquiere
The genus Hoplitoides has been established by von Koenen1 for certain
ammonites from the limestones of the Mungo in Kamerun; later Solger2
studied the same fauna and made the definition of the genus more precise.
Then Pervinquiere1 amplified this definition still more and distinguished
two groups within the genus Hoplitoides: the bicarinate and the monocar-
inate forms. The first group seems to be limited to the Turonian, the sec-
ond one to the Emscherian.
Among our material we find a few ammonites which very probably be-
long to the first group, the bicarinate Hoplitoides. The specimens are not
very well preserved and the generic determination is not entirely certain.
The external form corresponds completely with that of the Hoplitoides,
but the suture is much destroyed and scarcely permits recognition of the
general character of the line; this, however, coincides entirely with the
suture of the bicarinate Hoplitoides. The character of the suture on the
other hand shows that the specimens do not belong to Placenticeras, a
genus which externally is quite similar to Hoplitoides.
HOPLITOIDES aff. MIRABILIS Pervinquiere
PI. 19, figs. 1-3
1907 : Hoplitoides mirabilis Pervinquiere, Paleontologie Tunisienne, p. 218, pi. 10, fig. 3
Among the material placed at my disposition I found two relatively
complete specimens and four fragments which, according to their suture
and external form, belong to the so-called Pseudoceratites of the Creta-
ceous. The best preserved specimen shows the following features :
Shell discoidal, entirely evolute, with whorls of lanceolate cross section
truncated at the point, much higher than broad. The umbilicus is very
narrow, the umbilical wall is vertical and the umbilical border rounded.
The flanks are smooth, very little convex, nearly flat. The venter is flat
with a sharp shoulder on each side; on the internal whorl we observe on
both shoulders of the venter a sharp keel and the zone there is concave.
Jv. Koenen, Nachtr. Foss. Mungo i. Kamerun, p. 53.
2Solger, Mungokreide, p. 127.
226
University of Texas Bulletin
The suture is badly preserved, because all the specimens are corroded
on the surface, and rio suture could be made visible on the internal whorls.
We note a little ramified external saddle, which is rather broad and low;
the first lateral lobe is broad, shallow and ends in three points, those on
the umbilical side being longer than the one on the ventral side. Some
smaller ramifications exist on the sides of this lobe. The first lateral
i/^
VJ
Figure 7. Sutures, Neoptychites aff. xetriformis Pervinquiere (lower left hand corner)
and Hoplitoides sp. (other three).
saddle is broad and relatively high, and a secondary lobe divides it in two
parts. The following saddles are much destroyed and no longer show
their ramifications. The lobes are much shallower than the first lateral
lobe.
Dimensions :
Diameter 149 mm. (1) 119 mm. (1)
Height of the last whorl 76mm. 0.51 58mm. 0.49
Width of the last whorl 45mm. 0.30 34mm. 0.29
Diameter of the umbilicus 19 mm. 0.13 18 mm.? 0.15
Our specimens belong very probably to the genus Hoplitoides and to the
bicarinate group of it. Externally they resemble this group in an extra-
ordinary manner and especially Hoplitoides mirabilis Pervinquiere. Per-
vinquiere has united these forms, which distinguish themselves by a flat
venter even in a very advanced stage, with the Hoplitoides of the Emsche-
rian, which show a flat venter only in their youth, the venter in the adult
age becoming sharp or a little rounded. Only the study of a large and
> A New Ammonite Fauna of the Lower Turanian of Mexico 227
rich material could decide if it would not be better to separate these two
groups at least subgenerically. It was probably the want of sufficient ma-
terial which decided Pervinquiere not to separate the two Turonian species
from the rest of the genus. If such study should prove that all the species
from the Turonian belong to .the bicarinate group, it would be better to
unite them in a different species.
The main difference between our species and H. mirabUis consists prob-
ably in the larger diameter of the umbilicus, but our material is not suffi-
ciently well preserved to allow a more detailed comparison.
The two species of bicarinate Hoplitoides described by Pervinquiere oc-
cur in the lower Turonian ; one of them has also been found in the upper
Turonian (H. Munieri).
Eck1 cites with some doubt Hoplitoides mirabilis, or a similar form, from
the Turonian of Egypt. Woods2 describes a Hoplites Nigeriensis from Ni-
geria which he takes to belong to the bicarinate Hoplitoides. These spec-
imens occur in probably Turonian beds. In the same locality have been
found Vascoceras Gongilense Woods and Pseudaspidoceras sp. Woods
mentions that Hoplitoides has also been found in another locality of Ni-
geria.
Number of specimens : 2, and 4 fragments.
Age: Lower Turonian (Salmurian), upper horizon.
LAMELLIBRANCHIATA
AVICULA Bruguiere
AVICULA AGUILERAE sp. nov.
PI. 20, figs. 1-2, 11-12
The material from the upper horizon of the Salmurian of Cerro del
Macho contains a number of specimens of a large and well characterized
Avicula. Its features are :
Shell thin, of subquadrate form, nearly as high as broad, not very con-
vex ; the right valve is a little more convex than the left one. On the an-
terior side is a prolongation in form of an auricula which is not quite com-
pletely preserved but which certainly was not very long ; on the posterior
side we note a prolongation in form of a wing, with a precise limit be-
tween this wing and the rest of the shell. The auricula as well as the wing
!Eck, Turon in Aegypten, p. 382 and 386.
2Woods, Cret. dep. Northern Nigeria, p. 284, pi. 23, fig. 3; pi. 24, figs. 1-5; fig. 1
of the text.
228 University of Texas Bulletin
form with their superior border approximately the prolongation of the
cardinal border and do not elevate themselves above the beaks. The beaks
are small and pointed. The cardinal border is straight, long, and vertical
in relation to the longitudinal axis of the shell. The surface of the shell
is entirely smooth and shows only fine concentric striae of growth. All
our specimens are internal molds but some have preserved remains of the
shell.
Our very characteristic species resembles Av icula gravida Coquand.1 The
main difference seems to consist in the greater convexity of the valves in
this latter species, also in the different position of the beaks in relation to
the upper border of the auricula and the cardinal border ; but it is possible
that this last difference may be explained as an error of the draftsman,
because Coquand mentions expressly that neither the auricula nor the pos-
terior wing elevate themselves above the beaks. In every case our species
is nearly related to the African one.
Coquand mentions that his species occurs in the Turonian (Mornasian)1 ;
later on Peron2 corrected this determination of the horizon. He says that
he has always found this species in the Santonian, at the ^ase of the Se-
nonian, in the beds with Buchiceras and Hemiaster Fourneli. But not-
withstanding this correction it is possible that Coquand was right in his
determination of the horizon, because Pervinquiere3 also mentions that he
has found Avicula gravida in the lower Turonian. The species seems to
occur also in the Emscherian, from which horizon it is cited by Pervin-
quiere4 who has also found it at the base of the Senonian immediately
above the Turonian. The species thus probably lived from the Salmurian
to the Senonian; it is of course possible that the specimens found in the
different horizons really were different species, although these certainly
belong to the same group.
At first view, one might believe that our species are identical with Avi-
cula pedernalis Roemer1 but Avicula Aguilera does not have the singular
scars of that species, which remind us of those of Meleagrina. Roemer
has figured them and I have observed them also on a specimen from the
Vraconian of Arivechi, Sonora. The general form of Roemer's species is
also a little different from ours.
Number of specimens : 6.
Age: Lower Turonian (Salmurian), upper horizon.
Coquand, Geol. et Pal. de Constantine, p. 216, pi. 13, figs. 17, 18.
2Thomas et Peron, Hauts-Plateaux de la Tunisie, p. 241.
3Pervinquiere, Et. geol. Tunisie, pp. 101, 108.
4Pervinquiere, Et. geol. Tunisie, p. 115, 117, 151.
A New Ammonite Fauna of the Lower Turanian of Mexico 229
INOCERAMUS Sowerby
INOCERAMUS LABIATUS Schloth-aim
PI. 20, fig. 5
1813: Oxtracites labiatus Schlotheim in Leonhard's min. Taschenb. VII p. 93, fide
Geinitz.
1875: Inoceramus labiatus Geinitz, Elbthalgebirge II, p. 46, pi. 12 cum syn.
1893: Inoceramus labiatus Stanton, Colorado Form., p. 77, pi. 10, fig. 4; pi. 14, fig. 2
cum syn.
1903: Inoceramus labiatus Petrascheck, Inoc. a. Kr. Bohmens, p. 156.
In the upper horizon of the Salmurian of Cerro del Macho, Dr. Haar-
mann found four Inoceramus of which at least three are typical Inoceramus
labiatus Schlotheim. They are relatively small individuals but are en-
tirely identical with those from Parras, Mexico, and different European
localities. I have discussed this species extensively in Boletin 30 of the
Institute Geologico de Mexico; a detailed description of the specimens
found on Cerro del Macho does not seem to be necessary.
The occurrence of this species at our locality is of some importance
because the determination of the age of the Mexican Turonian beds up
to the present is entirely founded on bivalves, especially Inoceramus, and
this class of fossils is always stratigraphically of less value than the
cephalopods. My former determinations are now confirmed by the. oc-
currence of Inoceramus labiatus together with typical ammonites of the
lower Turonian.
Up to the present, Inoceramus labiatus has not yet been found in the
lower beds of our Salmurian ; it only occurs in the upper one, and even
there it is not very frequent. Of course we can not yet draw any con-
clusions from this distribution. The stratigraphical conditions of the
region of Mohovano should first be studied with care, larger collections
from the lower horizons should be made, so as to show if Inoceramus
labiatus really does not appear in those beds ; and finally the relation be-
tween the cephalopod beds and the shales with Inoceramus of other re-
gions of northern Mexico should be ascertained.
Number of specimens: 3 (4?).
Age: Lower Turonian (Salmurian), upper horizon.
230 University of Texas Bulletin
EXOGYRA Say
EXOGYRA HAARMANNI sp. nov.
PL 18, figs. 4-8
In the lowest beds of Cerro del Macho numerous specimens of an en-
tirely smooth Exogyra have been found. This species resembles to a
certain degree Ex. columba Lamarck but is not completely identical with
it._ Its character is :
Larger valve thin, very convex, especially in the central portion, thus
forming a kind of rounded crest which goes from the beak to the lower
margin. This crest gives the shell an asymmetric aspect because it is not
entirely in the center, but a little nearer the anterior margin ; this asym-
metry is particularly noted in large specimens and much less in juvenile
individuals. The beak is quite slender, spirally coiled at its point. The
valve is broad, without forming wings and without a furrow in any of
the sides. From the above mentioned crest the shell slopes rapidly toward
the anterior margin and slowly toward the posterior margin. The sur-
face is entirely smooth, showing only fine striae of growth and in a large
specimen there is an indication of two slight concentric ridges, certainly
produced by the manner of growth.
The smaller valve is nearly flat. In none of the specimens is the surface
entirely preserved and a detailed description of this valve can not be made.
Oar species resembles Ex. columba Lamarck but is much smaller and
never shows a radial ornamentation, and the rounded crest is nearer to
the anterior margin while in the European species it is nearer the posterior
one.
In its shape our species resembles still more Ex. columbella Meek,1
especially on account of the position of its crest, but the radial ornamenta-
tion of that species is entirely missing in ours.
Number of specimens : 12 and numerous fragments.
Age: Upper Cenomanian?, lower beds of Cerro del Macho.
EXOGYRA cfr. OLISIPONENSIS Sharpe
1850: Exogyra olisiponensis Sharpe, Secondary Distr. of Portugal, p. 185, pi. 19,
figs. 1, 2.
1911 : Exogyra olisiponensis Woods, Cret dep. Northern Nigeria, p. 278, pi. 20, figs.1-3.
cum syn.
In the upper part of the marls which we believe belong to the Ceno-
manian, Dr. Haarmann found a fragment of a large Exogyra. This
'Stanton, Colorado Form., p. 63, pi. 8, figs. 2-4.
A New Ammonite Fauna of the Lower Turanian of Mexico 231
species is distinguished by a moderately broad and coiled beak which slopes
quickly toward the anterior margin; this steep slope continues on the
valve itself, while toward the posterior margin the valve slopes in a very
regular curve. The ornamentation consists of radial, thick, and not very
numerous ribs. Where these are crossed by specially strong concentric
lamellae of growth, a kind of prolongations is formed which nearly re-
semble spines. The shell itself is very thick.
The specimen does not seem to be very nearly related to the Exogyra
with radial ribs, of the Mexican middle and upper Cretaceous (Ex. Whit-
neyi, Ex. costata, etc.) but much more to the varieties with few ribs be-
longing to the group of Ex. Olisiponensis from the border of the Med-
iterranean.
Our fragment is especially similar to an individual from the Cenoma-
nian of Wadi Am Rimpf figured by Fourtau1 ; this specimen shows a very
similar ornamentation.
Very similar also are some specimens from Deba Habe in Nigeria figured
by Woods ; these show particularly the strongly sloping region of the shell
toward the anterior margin.
Exogyra olisiponensis occurs in the Cenomanian as well as in the Turo-
nian. Many authors certainly take the species in a very wide sense and
we do not yet know if it is possible to separate specifically the form of the
Cenomanian from that of the Turonian. In general it seems to me that
our specimen resembles more the varieties figured from the Cenomanian
(compare among others Lartet, Geol. de la Palestine, pi. 11, fig. 1) than
those from the Turonian. With this view the layer in which our specimen
has been found coincides well; it occurs in the upper part of the marly
limestones directly below the Salmurian of Cerro del Macho. We have
considered these marls with some doubt as upper Cenomanian. Unfortu-
nately we do not know the exact stratigraphic position of the individuals
from Nigeria. Woods presumes that they come from the Turonian, be-
cause in Gongila, in Nigeria, not only typical cephalopods of the Turonian
(Vascoceras, Pseudaspidoceras, bi-carinated Hoplitoides) have been found,
but also specimens of Exogyra olisiponensis, while in Deba Habe only
Ex. olisiponensis has been collected. A solution of this problem is im-
possible for the moment, but there is the possibility that at Deba Habe the
Cenomanian might be represented by beds with Ex. olisiponensis.
Number of specimens: 1.
Age: Upper Cenomanian (?), upper part of the lowest horizon 6f
Cerro del Macho.
'Fourtau. Faune cret. d'fegypte, p. 287, fig. 5.
232 University of Texas Bulletin
GASTROPODA
TYLOSTOMA Sharpe
TYLOSTOMA aff. OVATUM Sharpe
PL 20, fig. 3
1849: Tylostoma ovat-um, Sharpe, On Tylostoma, p. 379, pi. 9, figs. 7, 8.
In the upper horizon of our Salmurian numerous specimens of gastro-
pods have been collected; among these Tylostoma or similar genera seem
to predominate. The greater part consists of internal molds which are
badly preserved. In some specimens we note that the labrum is thick-
ened on the inner side, thus these individuals very probably belong to
Tylostoma. It is very possible that there are different species in the col-
lection but in consideration of the bad state of preservation of the ma-
terial it is impossible, to distinguish them with certainty. The best speci-
men, as well as some less well preserved, has much similarity with T. ova-
turn Sharpe. Its features are:
Shell subglobose, of broad oval form, with a low spire of approximately
six coils, mouth suboval and relatively narrow, labrum having an inner
thickening. The surface is entirely smooth.
According to Choffat1 T. ovatum occurs in all the beds from the Bella-
sian to the upper Turonian ; it is thus not very surprising that a similar
form is found in our beds.
Number of specimens : 5 and probably numerous fragments.
Age: Lower Turonian (Salmurian), upper horizon.
ECHINODERMATA
HEMIASTER Desor
HEMIASTER sp.
PI. 20, figs. 6-10
In the lower marls of Cerro del Macho, Dr. Haarmann found a Hemiaster
which probably represents a new species. He found another specimen
loose below the hill which seems to belong to the same species, but it is
too badly preserved for determination. The features of the better pre-
served specimen are :
'Choffat, Syst. cret. Portugal II, p. 190.
A New Ammonite Fauna of the Lower Turanian of Mexico 233
Shell of small size, little convex, slightly polygonal in the ambitus, thin-
ning toward the back and toward the front, the greatest width lying far
in front of the center of the shell ; slightly notched in front and truncated
behind. The upper face is convex, the ambitus rounded, the lower face
is nearly flat, a little thickened on the plastron and slightly depressed in
the region of the peristome.
The impair ambulacrum lies in a relatively broad and moderately deep
furrow which begins in the apex and from these regularly widens toward
the ambitus, narrowing from there to the peristome; the furrow notches
the contour considerably. The zones of pores are composed of pairs of
small, nearly circular pores; the pores of each pair seem to be separated
by a slight thickening. The zone is wide and nearly smooth ; large tuber-
cles are missing there and only the fine granulation can be observed. The
zones of pores occupy less than half the furrow between the apex and the
ambitus. Farther on follow pores separated by larger intervals and of
an oblique position, arranged in such a manner that the pairs of the two
zones alternate. The exact number of these pairs could not be counted.
The anterior paired ambulacra are moderately large and of lanceolate
form ; they lie in relatively deep furrows. The poriferous zones are broad
and consist of pairs of elongated, nearly equal pores ; the pores of each pair
are connected by a very distinct furrow. The interporiferous zone is rela-
tively narrow and has not quite the width of one of the poriferous zones.
The posterior paired ambulacra are a little shorter than the anterior
ones. The poriferous zones consist of pairs of elongated nearly equal
pores; the pores of each pair are connected by a slight furrow. The in-
terporiferous zone is rather narrow and less wide than each of the porif-
erous zones. Outside of the petals the pores are smaller and the pairs
are separated by large intervals.
On the whole surface of the interambulacra we observe apparently cren-
ulated and perforated tubercles, enclosed by narrow areas and very near
together; they are stronger on the anterior portion than on the posterior
one. In the interporiferous zones of the ambulacra of the upper face,
tubercles do not seem to exist. In the ambulacra of the lower face tuber-
cles are infrequent, while the interambulacra of the same face are densely
covered by tubercles, especially the plastron; they decrease in size from
the center toward the outside. The whole surface of the shell is covered
by a fine granulation.
The impair posterior inter-ambulacrum of the upper face has a sharp
crest which is higher than the apicial apparatus. The anterior interam-
bulacra of the same face show much less pronounced crests; the lateral
interambulacra are flattened on the center, the flattened zone being lim-
234 University of Texas Bulletin
ited by well marked borders. These margins and the crests of the other
interambulacra give the polygonal contour to the figure of the shell.
The peristome is small and of subpentagonal form. Its position is ex-
centric toward the front; the lip is rather prominent. The periproct is
not well preserved, but is of oval form and lies in the upper part of the
posterior face. The apicial apparatus is relatively large, the two posterior
pairs are widely separated from the anterior ones ; the details can not be
clearly recognized.
Dimensions:
Antero-posterior diameter 27.8 mm.
Transversal diameter 27.3 mm.
Height 19.0 mm.
Distance between the apex and the posterior margin 16.2 mm.
Our species is not very characteristic but I have not found one with
which it might be identified entirely. It resembles to a certain degree
Hemiaster Meslei Peron et Gauthier,1 but in this species the posterior am-
bulacra diverge much more than in ours, the contour is more notched in
front, the furrow of the impair ambulacra is much narrower and deeper.
As we have not more than one well preserved individual I only describe
and figure it without giving a new name to this species, or identifying it
with a known one.
Number of specimens: 2.
Age : Upper Cenomanian ( ?) , lower horizon of Cerro del Macho.
lCotteau, Peron et Gautheir, Ech, foss. de 1'Algerie IV, p. 102, pi. 2, Igs. 5-8.
PLATE 12
Metoecoceras, Fagesia, Mammites
236 University of Texas Bulletin
Metoecoceras, Fagesia, Mammites. Plate 12
Figures 1, 2, 3. Metoecoceras sp. nov page 205
Upper Cenomanian (?) or lower Turonian. Cerro del Macho, Hacienda de Moho-
vano, Coahuila.
Fig. 1. View from the opposite side from Figure 3.
Fig. 2. Venter of the same specimen.
Fig. 3. Side view.
Figures 4, 7. Metoecoceras aff. Whitei Hyatt page 203
Upper Cenomanian (?), lower horizon of Cerro del Macho, Hacienda de Moho-
vano, Coahuila.
Fig. 4. Venter.
Fig. 7. Side view.
Figure 5. Fagesia Pervinquieri sp. nov page 212
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Venter and cross-section.
V
Figures 6, 8. Mammites mohovanensis sp. nov page 206
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Fig. 6. Cross-section and venter.
Fig. 8. Side view.
University of Texas Bulletin No. 1856
,'. 'Flate 12
PLATE 13
Pseudaspidoceras
238 University of Texas Bulletin
PLATE 13
Pseudaspidoceras Plate 13
Figure 1. Pseudaspidoceras aff. Pedroanum White sp page 209
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view.
University of Texas Bulletin No. 1856
Plate 13
1
PLATE 14
Fagesia, Vascoceras
240 University of Texas Bulletin
PLATE 14
Fagesia, Vascoceras Plate 14
Figure 1. Fagesia Haarmanni sp. nov page 211
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
View of the other side of the specimen figured as Fig. 2, PI. 15.
Figure 2. Fagesia Haarmanni sp. nov page 211
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Cross-section and venter of specimen figured as Pis. 15 and 14.
Figure 3. Fagesia Pervinquiri sp. nov page 212
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view of specimen figured on PI. 12, fig. 5.
Figure 4. Vascoceras n. sp. ex. aff. V. adonense Choffat page 214
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Cross-section and venter.
University of Texas Bulletin No. 1856
I M.,..- 14
PLATE 15
Pseudaspidoceras, Fagesia, Vascoceras
242 University of Texas Bulletin
PLATE 15
Pseudaspidoceras, Fagesia, Vascoceras Plate 15
Figure 1. Pseudaspidoceras aff. Pedroanum White sp page 209
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Cross-section and venter.
Figure 2. Fagesia Haarmanni sp. nov page 211
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view.
Figures 3, 4, 5. Vascoceras aff. Gamai Choffat page 216
Lower Turonian, probably from upper horizon. Cerro del Macho, Hacienda de
Mohovano, Coahuila.
Figs. 3 and 5, view of both sides.
Fig. 4. Cross-section and venter of the same specimen.
University of Texas Bulletin No. 1856
Plate IS
PLATE 16
Vascoceras
244 University of Texas Bulletin
PLATE 16
Vascocera* Plate 16
Figures 1, 2, 3, 4. Vascoceras Angermanni sp. nov page 217
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Fig. 1. -Side view.
Fig. 2. Cross-section and venter of specimen figured on Fig. 4.
Fig. 3. Cross-section and venter.
Fig. 4. Side view of a larger specimen.
University of Texas Bulletin No. 1856
Plate 16
•
PLATE 17
Vascoceras
246 University of Texas Bulletin
PLATE 17
Vi.coceras Plate 17
Figure 1. Vascoceras Angermanni sp. nov , page 217
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view of a large specimen.
Figure 2. Vascoceras n. sp. ex. aff. V. adonense Choffat. page 214
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view of the specimen figured on PL 14, fig. 4.
University of Texas Bulletin No. 1856
Plate 17
1
f
w
PLATE 18
Vascoceras, Neoptychites, Exogyra
248 University of Texas Bulletin
PLATE 18
Vascoceras, Neoptychites, Exogyra Plate 18
Figures 1, 2. Vascoceras Mohovanense sp. nov page 219
Lower Turonian, lower horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Fig. 1. Side view.
Fig. 2. Cross-section and venter.
Figures 3, 13, 10. Neoptychites aff. Cephalotus Courtiller. pags 221
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Fig. 3. Side view.
Fig. 13. Cross-section and ventef of the external whorl of the same specimen.
Fig. 10. Cross-section and venter of the inner whorl.
Fiures 4, 5, 6, 7, 8. Exoyna Haarmanni sp. nov page 230
Upper Cenomanian (?). Lowest horizon of Cerro del Macho, Hacienda de Moho-
vano, Coahuila.
Fig. 4. Side view.
Fig. 5. Side view.
Fig. 6. Small valve.
Fig. 7. Large valve.
Fig. 8. Large valve.
Figures 9, 11. Neoptychites aff. Xetriformis Pervinquiere page 223
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Fig. 9. Cross-section and venter.
Fig. 11. Side view.
Figure 12. Vascoceras sp PaSe 218
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view.
University of Texas Bulletin No. 1856
P'«te 18
12
PLATE 19
Hoplitoides
250 University of Texas Bulletin
PLATE 19
Hoplitoides Plate 19
Figures 1, 3. Hoplitoides aff. mirabilis Pervinquiere page 225
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Side view of two specimens.
Piure 2. Hoplitoides aff. mirabilis Pervinquiere page 225
Lower Turonian, upper horizon. Cerro del Macho, Hacienda de Mohovano, Coahuila.
Cross-section and venter of specimen figured on Fig. 3.
University of Texas Bulletin No. 1856
f
PLATE 20
Avicula, Tylostoma, Exogyra, Inoceramus, Hemiaster
252 University of Texas Bulletin
PLATE 20
Avicula, Tylostoma, Exogyra, Inoceramus, Hemiaster. Plate 20
Fiures 1, 2, 11, 12. Avicula Aguilerae sp. nov page 227
Lower Turonian, upper horizon. Cerro del Macho, Hacienda del Mohovano, Coahuila.
Fig. 1. Left valve of specimen.
Fig. 2. Left valve.
Fig. 11. Cardinal margin of same specimen.
Fig. 12. Anterior side.
Figure 3. Tylostoma aff. ovatum Sharpe page 232
Lower Turonian, upper horizon. Cerro del Macho, Hacienda del Mohovano, Coahuila.
Figure 4. Exogyra cfr. olisiponensis Sharpe page 230
Upper Cenomanian (?) Lowest horizon of Cerro del Macho, Hacienda del Moho-
vano, Coahuila.
Figure 5. Inoceramus labiatus Schlotheim page 229
Lower Turonian, upper horizon. Cerro del Macho, Hacienda del Mohovano, Coahuila.
Figures 6, 7, 8, 9, 10. Hemiaster sp. . . . page 232
Upper Cenomanian (?). Lowest horizon of Cerro del Macho, Hacienda del Moho-
vano, Coahuila.
Fig. 6. Front.
Fig. 7. Posterior side.
Fig. 8. Left side.
Fig. 9. Lower face.
Fig. 10. Upper face.
University of Texas Bulletin No. 1856
Plate 20
12
INDEX
italics d«poie description of species.
Abbreviations, tables of fossils 46, 61, 55, 67
Acanthoffra.1 201, 221
cfr. Choffati KOKSIUM 197
neptvni ... 197
prmodosoidet u. L. & f. .. 67
«J>. 44
*i<l<r/,-/n<ili Bou'e, Lemoine and Thevenin
67. 202. 203
vieinale Stoliczka 202
wwlAenae n. sp. wj, 150
Acompiocera* .201
Adkins, W. S. 12, 1J6, 147
Africa, northern 42
limonite and pyr'ts tauna "f 64, 66
Turonian of _ 20$. 209
AKuilcra, Jose G. 190, 192
Albian, correlation of . 10
fauna of 64, 66, C6
Algeria 45. L'14. 223
fauna of 66, 194
Salmurian of .194
Algiers 6«, 189
Alpine- Terlinpua road 60
Amberleya graysonensis . _/.?;". lf.0
Ammonite fauna, Lower Turonian . 179
Ammonites, description of species Si, et. seq.
pyritic or limonitic 44, 59, 60, 64, 66
tabulation of 01
Ammonites acceleration Hyatt 201
arnesennis Choffat 189, 219
conciliates Stoliczka 208
GeslianuK d'Orbigny 202, 202
gibboaum Hyatt 201
Harttii Hyatt 198
Kanabense Hyatt 201
Kotoi Yabe 188
leonensis Conrad 211
Loewianvs White 208
offaccinatuH White 199, 221
pedroanus Kossmat 210
pedroanus White 187. 198,~~199
Swallovi Shumard 200
Whitei Hyatt I~~"201
Anrhura mttdffeana White 139, 169
Ancycloceras bendirei n. sp. 70, 170
linratiu Gabb 71
inatheronianum d'Orbigrny 71
Angermann, Dr. Ernst 179. 184. 217, 218, 223
Aptian, correlation of 10
Aptian-Gault 199
Aptien age __ 42
Aquitania, cephalopods of 197
Area 28, 26, 28, 29, 32, 83
VOfAltaflMil r. sp. 54, IS1, 168
Arivechi, Sonora 26, 228
Armstrong Iron Works 47
Asia, Turonian of 208
Asterisk, explanation of 46
Asteroidea 95
Atoka. Oklahoma 22
Austin, Texas 19, 68, 68
Australia, fauna of 198
Avicula aavUerac n. sp. 190, 2S7, 252
rjravida Coquand 180, 190, 228
pedemalis Roemer 228
Hacvlitea comanchenaia n. sp. 74, 152
Bailey County, Texas ._ 25
Bandera road 59
Baptist Seminary, Fort Worth .. 61
Barroisiceraa ( T) Fleuriausianum d'Orbigny 197
Itrlemnites fibula, Forbes 67
Bend arch 14
Bennington, Oklahoma 17, 19, 28
Benton formation _200
Berry, E. W. 44. 146
Bibliography. Ammonite Fauna of Lower Turo-
nian of Mexico 180-183
Weno and Pawpaw Formations of Texas
Comanchean 146-147
Blayac. J. 66
Blue Mound, Tarrant County 21, 83, 65
Blum, Texas 12, 28, 26. 40, 54
Rochianitee Lory 75
Bohemia, fauna of 197
Bokchito, Oklahoma 17, 19, 28
creek . 29
formation 28, 29, 40
Bom Jardin, Brazil ^199
Bom Jesus, Brazil 199
Boese, E. 20, 72. 146
Boule. M. 67. 180, 202
Branca, W. , igo
Brazil, Salmurian fauna of- .198, 200, 210, 214, 221
Brazos-Colorado divide 16, 22, 24
Brazos River 21, 41, 64
Urewster County, Texas 60
Bruder, G. 197, 207
Bryan County. Oklahoma 16. 27
thickness of formations in 15
Ruchiceras 228
"Buchiceras" SwaUovi Shumard 202, 206
Buda fauna 43
formation 42, 62
Buff marl 37
Burleson, Texas ._ 17
Caddo, Oklahoma 22, 29
Caddo limestone of Taff 28, 40
Cajamarca, province of 199
Camacho, Zacatecas £0
Vraconian of 200
Camp Bullis, Texas 14
Carillo. Mexico 188, 190
Cedar Creek 64
Cedar Hills " 31
Cedar Mills, Texas .__12, 19
Celendin, Peru '199
Cenomanian 179, 190, 192, 200, 280, 28l"234
correlation of jo
f?u?? — --------------- '^e^ 67
of Diego-Suarez 208
of Saxony 201, 206, 206
of United States ____• 205
Cephalopoda 68
Cerithium 29
Cerro del Macho 179, 190, 191, 192, 214, 218
Cenomanian of 206, 230, 284
fauna of 192, 200, 203
fossil-bearing beds of ...183
marls of 282
Salmurian of 193, 211, 216, 227, 2297281
Turonian of 208, 209
Cerro de Muleros, N. M. _ 16, 17 18 19
20. 21, 22, 28. 24. 25, 36, 41, 42, 191, 192, 200
Chihuahua___ ig, 28. 183. 191
Choctaw County. Oklahoma 26, 27
Choffat, P. 186. 189, 198, 198, 218
Christiansen, F. 68
Chudeau, R. .__!»«
254
University of Texas Bulletin
Cia. Perforadora Mexicana 180 EnaUaater 111
Cinula washitaensis n. sp 14S, 168 bravoensi« Boese 17, 41, 114, 164
Cintdia sp. 54 sp. aff. texanua (Roemer) 31, 114
Cleburne, Texas 25 wenoensin n. sp. IIS, 158
Coahuila, Mexico 179, 183 Engonoceras . 26, 31, 32
Cobb Brickyards, Fort Worth 47 serpentinum (Cragin) 84, 166
Codiopsis sp. aft. doma 44 sp. 54. 85, 156
Coke County, Texas 26 Epiaster 84
Colorado formation 185, 200, 205 Aguilerae Boese 109, 158
Comanchean sea in Texas 44 subobesiu n. sp. 110, 170
Comanche Peak, Texas 17, 24 wenoensis n. sp. 105, 160
Comanche series, thickness 16 Escalon, Mexico 183
Comptonia wintoni n. sp. 97, 162 Etheridge, R., Jr. 198
Constantine, provence of 65 Europe, limonite and prite fauna of 64
Cooke County, Texas 9, 12, 20, 22, 27 Exogyra arietina 18, 19, 81, 41, 42
thickness of formations 15 cartledgei 18
Coquand. H. __194. 228 c*r- olisiponensis Sharpe 192, t30
Corbula 29, 31, 32 columba Lamarck 199, 236
basiniformis n. sp. IM, 166 columbella Meek 230
HUnralis n. sp ___29, 133, 16B costata 231
Correlation of formations 10 Haarmanni n. sp. 185, tso, 248
Cotteau, G. 146 olisiponeneis 231
Cragin. F. W. 46, 146 8"' aflf- arietina Roemer Its
Cretaceous, Mexican 231 texana 16
Crustacea, tabulation of pyrite and limonite 62 Whitneyi 17, 42, 231
Cuesta de Huanambra, Peru 199 Exposures of Pawpaw 47
Cuesta de Huanyanba 199
Cummins, W. F., and Dumble, E. T 18 Facies 16
Cvphoftoma volanum Craprin los Fagesia 196, 200, 211
Cyprimeria washitaensia n. sp 134, 166 Boucheroni Coquand 197
Haarmanni n. sp. 187, 111, 240
Dagger, explanation of __ _ 45 Kotoi 198
Dakota flora, age of _ 44 rudra. Stoliczka 187. 198. 213
Damergou __196 superstes Kossmat 186, 187, 197, 198, 212
Davis. John _ __ 68 tevexthenxis Peron 186, 187, 188, 197, 212
Deba Habe, fndia _ ' 231 Fallot, J. E. 65
Decatur, Texas .. " 14 Feli* and Lenk 25
Del Rio, Texas _ " _58~ 69 Fhlk' Texas 16- 23. 24, 54
Del Rio clay __17, 18, 19 41 63 56 69 Fin'ay Mountains, Texas 16. 25
fauna of ' 68 "5*5 26' 42
limonite and pyrite fauna__ 61 boesei n. sp. - *.;, 150
Denison, Texas__17, 19, 20, 22, 24, 30, 47, 54, 55, 68 bosquensis n. sp. . ...S7, 150
Denton County, Texas 19, 12, 17, 30. 35, 37, 54 Fort Stockton, Texas _ 16. 24
thickness of formations... . 16 Fort Worth, Texas
Denton clay, fauna of 55, 60, 62 -12' 13' 14' 17> 20' 2L 24. 32- «• 51
limonite and pyrite fauna of 43, 61, 62, 63 Fort "orth formation ..21, 2:
marl 41, 46, 53, 64, 62 facies of
Descriptions of species __68, et. seq geosynchne
Desert sandstone _ 198 limestone 22, 62
Desmoceras brazoense 23 Fossil-bearing beds of Cerro del Macho 183
Diego-Suarez . ..203 Fossils, pyrite 9, 83, 42, 44. 53. 60
Diener, C. _ 197 Fourteau, R. 231
Dieulefit France _ __ 65 France, Salmurian fauna of...
DouviUeiceras mammilar'e '.'. "_ 43 Turanian of 212. 223
Duck Creek marl... ...42, 53, 54, 62 Fredericksburg division .
fauna of 54, 60 ^f1?8 —
limonite and pyrite fauna of 43, 61, 62, 63 _ thickness of
upper and lower facies 22 F«tsch, A. ..196, 197, 208
Dumble. E. T. 146
and Cummins, W. F. 18 Gabb, W. F. 25
Durant, Oklahoma 17, 28, 29 Gainesville, Texas, 12, 17, 19, 20, 25, 31. 32. 47, 51, 54
Gainesville Brick Company 31. 36. 47, 51
Eagleford shales 1 43, 199 Gastropoda 137, 191, 232
Echinodermata 232 Gastropods, tabulation of pyritic or limonitic.. 63
tabulation of limonite 61 Gatesville. Texas 14
Echinoidea 101 Geinitz. H. Br. 202
Echinoid fauna of Washita formation 52 Georgetown, Texas 12, 14
of Weno formation 44, 52 limestone 19, 20, 21, 41, 59
Eck, O. 180, 195, 197, 227 Geosyncline, Fort Worth formation 13
Edwards formation _- 24 GerviUiopsis invaginata 34
facies 24. (White) Ill
Egypt 214, 218. 227 Ginger shale 36
ammonites from 180 Glenrose formation 14, 43
fauna of 196 Globiconcha sp 140, 168
Salmurian of 193, 196 Gongila, Nigeria .-231
Turonian of 188, 190 Goniopygus sp. 102
Ellenburger limestone 13, 14, 16 Goodland. top of
El Paso, Texas 21, 24 fauna of 62
Emscherian, the 190, 196. 200, 205, 225, 226, 228
A New Ammonite Fauna of the Lower Turanian of Mexico 255
Grayson County, Texas 9, 27
thickness of formation in 15
Grayson formation 17, 19, 29, 41, 58
facies of 17
fauna of 48, 66. 60, 63
limonite and pyrite faunae of 61, 62, 63
Graywacke 14
Gryphea 29, 86
mucronata 18, 19
dilatata 20
washitaentit . 21, 28, 29, 41
Grossouvre, A. 146, 223
Guillemain, C. 196
Haarmann. E. ...180. 188, 184.
190. 191, 192. 206. 208. 211, 217. 218, 229. 230
Hacienda del Mohovano 179, 188
Hamites 28. 26. 28
quadrinodofuf Jimbo 71
simplex 42, 69
»P 54
sp. aff. armatvs Sowerby 69
tinaira Adkins and Winton gg
llamulina worthengis n. sp. 71, 162
Harbort, E. 196
Haslet. Texas 21, S3, 51, 65
Haug, E. 64, 146
Heinzia 201
Helicocryptus mexicanvs 41
Boese 189
Hemiaster 180, 232
Coirini Clark 17, 42, 114, 168, 191
Fmirneli 228
Meslei Peron et Gauthier 234
sp. tSt, 252
riovistae n. sp. Its, 160
Hill County, Texas 20, 85
thickness of formation 16
Hill. R. T. 16, 46. 146
Hillsboro. Texas 13
Holanter sp. aff. simplex Shumard 104
tvbglobomw 48
Holectypus limitis 88, 108
Homarua 62
Hood County, Texas 17
Hoplitoides 189. 196. 225. 231
aff. mirabilis Pervinquiere tts, 250
ingens v. Koenen 199
mirabili* Pervinquiere 190, 226
Munieri 190, 227
niaerientw 227
sp. 226
Hoploparia 62
Horizons, fossil 12
Hugo, Oklahoma 19, 24, 29
Huronian slates 14
Hyatt, A. __ 201, 202
India, fauna of _- 198, 200, 209, 212
Inoceramus Sowerby 229
hercynicus Petrascheck 179, 191
Inl'itituH Schlotheim
179. 186. 190, 192. 200. tS9, 252
cycloide* 191
Institute Geologico de Mexico 229
Jack R. L. 198
Japan. Turonian fauna of 198
Johnson County. Texas 9, 20, 85, 61, 54
thickness of formations in 15
Johnston, A. W. . ._ 14
Juarez, Mexico 191, 192
Kamerun, Africa 189, 225
fauna of 196
Kanab Valley, Utah 206
Kent, Texas 16, 18, 25, 35
Kiamitia formation 23, 40, 68, 54
conglomerate
clay, fauna of .. M
facies ""•*' 91
Kidney shale ""."."
Kingena ~™S~f ~ 38
Koenen. A. von ~~~. ' 225
Kossmat, A. igg, 198~"2(>2~"2087"224
-191
Lamellibranchia _______
Lamellibranchiata ____ """227
Lamna _________
Lartet, L. ........... ~" •"£
Laube. G. C. . — ...... _•___. ""197" 207
Lemoine, P. . ""«V ion o
Leander. Texas .:~~~"~:. T..' 18°' 2Jf
Lensing, in Comanchean formations""
Leiocidaris . _____________ 2!)"~ini
Leon Springs. Texas ..
Liddle, R. A. ____________ ~
Limonite and pyrite fauna of Africa"""
of Europe ____________________
of Madagascar .
of Texas ........... -----
summary of ...
Lisson, C. I ....... . a
Lithological changes .. ' ,«
Loew. Oscar _________ """208
Love County, Oklahoma
Lunatia sp. ---------- '"il'Ttn" tfta
McLennan County, T«as "-Tr:.".".".'.".'!! 86, 64 66
Madagascar ---------- 209 9nv
.
pyritic fossils of
209
2°2'
Mainstreet limestone .. ~rrr~™""48,"V7","BV 59
facies ~_ f£- }jj
fauna of
sandstone in
Mammites ~" " 2o6""221
cfr. cranaitetta Stoliczka "197" iqs
conciliates ""107 }
Fntech i"."~~ lm
Steliczka _ ~"fBR~~9n7~~on<
-186. tot, 236
Laube et Bruder. emend. Petrascheck""" "_tna
Mohovanenng n. sp. 186. toe. 220, 286
nodosotden Schlotheim. .186, 197, 198, 199 207 208
var. Afra Pervinqniere ' 199
Mantelliccras 201
Mariscal Mountains, Texas fg~ 41
Marshall County, Oklahoma ___IH"
thickness of formations
Medina County. Texas " 68~ 69
Meleagrina ' ...is
Metoecoceras .. 19l" Mn""9ni""->n9
aff. Whitei Hyatt
Geslianum Petrascheck
sp. nov. . igs> 192, t'os, 2S5
^VIMei* 2°2'' 20S
Metopaster 'hortensae Adkins" "•nd'wfnton "" 97 162
Mexico _ a-,*
and West Texas — IIIIII_II"i; 41
Mornasian 228
Mortoniceras
n- »P- 1™"™-~ ;il»ir"l60
worthense 43
Mungo region, of Africa "_19e""226
Myra, Texas _!.!____ 13
Nacreous fossils, Weno 26, 44. 64
-
NautHiu sp. gg
texanua fc .r, ., j
Neoptychites -"-"-V."."."_".V."."l967200,' 221
aff. cephalotus Courtiller 189, ttl. 248
aff. xetriformix Pervinquiere 179, US, 226 248
erataus Solger igg
telingaeformis Solger " 139
256
University of Texas Bulletin
Telinaa Stoliczka 189, 198, 223
xetra 224
xetriformis 189, 222, 224
Nerinea sp.
Nerita sp. ***• 168
Neritina sp. «». 168
Nigeria, fauna of 196, 209. 214, 227, 231
Nodosaria texana 18, 19, 28, 32, 34, 41, 146, 170
Noetling, F. 146, 197
Noland's River
North Central Texas
North Denison sands _.:
Northern Europe, fauna of -
France, fauna of
Germany, fauna of
Tunis, pyritic fauna of 66
Nucula —29. 31, 3:
nokonis n. sp. — 118, II
wenoensis n. sp. -. . — 1*0, 168
Oklahoma 40
Opal, Zacatecas .—60, 191
Ostrea(Alectryonia}quadrir>licata Shumard _
carinata
carinata ? Lamarck .
columba major — • 193, 194
foisseyi Lemoine _. 6|
marcoui
quadriplicata 20, 28, 29, 31, 32, 36, 41
sp. aff. diluviana Linnaeus --
subovata
Ostreidae
Oxyrhina
Pachydiscus peramplus _
Pachymya
Paleontology
Palestine, fauna of _
Paluxy sand
Parker County, Texas, thickness of formation-- 16
Parras, Mexico 229
Pawpaw formation 9, 41, 42, 43, 51. 53, 60, 62
clay facies of 32
correlation of 1°, 40
facies of 11. 20, 26. 27
fauna of 44, 45, 60-63
fossils 9, 10
ironstone of
limonitic and pyritic fauna of 61-63
lithology 26, 27
location of outcrop --9, II
marl facies S<
thickness 26, 26, 33
changes in 10, 12
sandstone facies
shales 45
stratigraphy
Pecos, Texas 1?
Pecten - 29, 33
georgetownensix (Kniker) _
inconspicuus Cragin 123, 170
mbalpinus 17, 29, 31
Pedinopsis symmetrica (Cragin) .
Pelecypoda
Pelecypods, pyritic or limonitic, tabulation of — 63
Peltastes sp. ._.102
Pennsylvanian strata .--18, 14, 1
Pentaceras ainericanus n. sp. 3.9, 162
Pentagonaster teitnsis Adkins and Winton— S5, 162
Peron, A. «6, 194
Peru, Salmurian fauna of _. . — 199, 200, 214
Pervinquiere, L. 42,
45, 64, 66, 146, 189, 194, 196, 208, 212, 221, 222
Petrascheck, W 186, 186, 197, 201, 202
Petrographical horizons 183
Phyllocr.raa forbexiatium d'Orbigny : 67
diegoi Boule, Lemoine and Thevenin 67
Pinna 33
yuadalupe Boese 41
Placenticeras 226
Placonmilia 63
bravoensis 41
mexicana 41
gp. 41
Plicatula sp. 29
Polytechnic well. Fort Worth 13
Porto dos Barcos 199
Portugal, fauna of 196, 209, 214, 217
Turonian fauna of, 186, 187, 188, 193, 212, 218, 221
Pre-Cambrian strata --. 18. 14, 16
Primrose, Tarrant County 54
Prionotropis 202
Woolgari 197, 211
Protocardia 34
multistriata 20
«p. aff. mltistriatum (Shumard) 1X6, 168
sp. aff. texana 20
texana 17
Protozoa 145
Province of Sergipe, Brazil 199
Pseudaspidoceras 196, 198, 200, 231
aff. Footeanum Petrascheck 186, tOS
aff. pedroanum White 187, 209, 238
Footeanum Stoliczka 186, 198, 199, 209, 210
pedroanum White 210
aalmuriense 197, 209
sp. 227
PfteudotisBotia Douvillei 197
Ptychoceras 69
Ptychodun ' 63
Puzosia Austeni 197
Pyrite ammonites 42, 55, 66, 58, 69, 60-61, 64-67
fauna, comparison of 53
of North Texas Comanchean 53-67
of Pawpaw formation 44.47-53
summary of 60-67
Pyritic starfishes 54
Quarry limestone 29, 31, 32, 35, 36, 37
Quihi, Texas 68, 59
Red River J 64, 55
Red River valley 19. 20, 21, 27, 36
Reed Plateau, Texas 59
Regularia 62
Remondia 32
Remondia? acuminata (Cragin) 1S6, 160
Rhone basin 65
Richardson, G. B. 147
Riovista, Texas 12, 20, 25, 51
Ritter, Frederico 183, 211. 218
Roanoke, Texas 17, 18
Roberts, Jno. R. 41
Roemer, F. 228
Round Rock, Texas 19
Rudistid facies 17, 24
Runnels County, Texas 25
Sahara desert, the 214
Salenia sp.
Salenidae 62
Salmurian, faunas of, 186, 199, 194, 195, 196, 208.
211, 212, 213, 215, 217, 218, 219, 227, 228, 231
Santonian 228
Saumur, France 189
Saxony, Cenomanian of — 186, 209
fauna of 197
Saxony-Bohemia, Sa'murian of 200
Sayn. G. 64, 147, 202
Scapkites .-26. 2:
aefjualia 42, 67
Hilli Adkins and Winton '9, 162
sp. —54, 69
sp. aequalia 43
wortkenftis 16
Sch'agintweit, O. 199, 200
Schlvcnbachia 211
A New Ammonite Fauna of the Lower Turanian of Mexico 257
ftobieiuu _.> 48
in/lata - 42
manteUi 48
sp ._ 17. 23
trinodosa 23
rarian* 43
wenoennif n. %v. 89, 160
wint&ni n. sp. 90, 164
Schweinfurth. collections of ...195
Sellards. E. H. 14. 147
Senonian ...179, 190, 1»9, 200. 228
Shafter, Texas 16. 18
Sharks, remains of 68
Sheffield. Texas 16, 24
Shuler. E. W. 62
Sierra Blanca. Texas 16, 26
Sierra Mojada. Mexico _ 183
Sladen. P. 147
Slate, Pre-Cambrian _ 14
Solirer. Fr. 194. 196. 198, 226
Solitario. the _ 68. 60
Sonora. Mexico 18
South America, Salmurian fauna of 198. 208
South Bosque. Texas _ 19, 68
South Bosque River 5V
South Central Texas 40
Southern France, fauna of 197
Sahara, fauna of 196
Spain __^ 214
Spencer, W. K. 147
Stanton 201, 205. 206
Starfishes, pyritic 54
Ste-nonia sujifrnut iCnmini 62
Stephanocera* 212
Stephenson, L. W. 20. 36. 40. 46
Stoliczkaia 202
Stoliczka. F _. 207. 223. 224
Stratitrraphy 13. 183
Sugar Loaf Mountain. Bryan County. Okla-
homa „ 28, 29
Sulphur Creek _. 29
Sycamore Creek _-_33. 38. 39, 47. 51
Syria, fauna of 197
Szjanocha. L. 43, 147
Tah'e of fossils:
of Del Rio clay 58-69
of Denton clay _.i. 66
of Duck Creek formation ._ 55
of Grayson marl 67-68
of Pawpaw formation 51-52
of Weno formation 48-50
pyritic and limonitic _61-66
Taff. J. A. 29. 30
Tarrant County, Texas _ _
9, 12. 20. 23. 33. tt. Yl.'l't. 55
thickness, of formation ._ 15
Terliniroa. Texas ._ 16, 58, 59
Creek _ 60
Thevenin, A. 67, 202
Thicknesses, of Comanchean ~~. .. 15
ThomajtitfK " 196
Tishominfro, Okla
Tifiaotia spp. 44
Trapichc das Pedras Velho, Braiil... !IIl99
Trigonia 29, 32. 179
Trinidad mine ' go
Trinity division, thickness of ] '~_ 15
TrofhoKmilitt gjj
Trochus laticonicu* n. sp. ~~lYs~~168
Tucumcarii. N. M. __18 '0
Tunis 46, 66. 187. 190. 196, 212. 214. 221. 223 ' 2~> I
fauna of 194
Turonian .-205. 2«fi 208
209. 212. 213. 215. 217, 219. 221. 223. 226' 228
correlation of 10
of Mexico V 179 <"«>
Turonian. Lower, Ammonite fauna of-.. '_ 179
TurninK point of outcrop Id
northern, at Orlena, Cooke County 27 '
southern, Bexar County 19, 21, 24
Turrilites 26, 28
bo8iiuvnnix n. sp. 76. 164
brtuotnn* 19, 31, 38, 41
sp. 33. 64. 69. 7S, 154
worthenttig Adkins and Winton 78, 154
Turritflla 28. 29
t/rayttonennia n. sp. ~14<), 168
•p. 54
U'orthcnnin n. sp. 141, 168
TyloKtoma ovatuin 232
Type collection 68
Udden. J. A. .. 14
Union Station, Denison " 47
United States, Salmurian lacking in 199
Turonian fauna of 199
Utatur trroup, of India 187, 212, 224
Valangian 61
Voscocxro* 196. 213, 221, 231
adonenne 186, 187
aff. adonense 214, 216
aff. arnesenae Choffat 214
aff. Gamut Choffat 214, 216. 242
amieirense Choffat 199
Angermanni 219
sp. nov. 214, 216, Sir, 244
Caudini 196
Douvillei 214
Durandi 193
ex. aff. Gamai Choffat IIIIIlSS
Gamai 213. 216
Gongilentte Woods 227
Harttii Hyatt ". illzil
harttiiforme 214
KoKsmati 179
mohovanenae n. sp. 189, 214, SIS, 248
Mundae 216
n. sp. ex. aff. V. adanense Choffat 114, 240
liolynioriikum Pervinquiere 189. 199, 220. 221
sp 189. tlS, 248
Hubcanciliatum 214, 220, 221
Venericardia wenoennis n. sp. 125, 160
Von Koenen, A. 225
Vraconian. correlation of 10
faunae __ 23, 42"".~66,~~66~, 67
of Arivechi, Sonora 228
Waco __67, 58
Wadi Am Rimpf ...231
Walcott. C. G. __205
Washita division 42, 46
fauna of 43. 44, 52, 64. 60-62
thickness of 15
Weno formation 9, 20, 33. 43, 46, 61, 62
correlation of 10 4(1
facies n, 20, 26, 27
fauna 45.50
fossils 12
ranjre of 46
table of 48-60
litholoiry 26. 27
location of outcrop 9, 10
sandstone in , .' 20
stratigraphy of ~ 13
thickness of 26. 26
changes in 10, 12
West Texas 41
and Mexico ._ 41
Whitney. F. L. 102 147
Winton. W. M. 9, 28, 32. 33. 146. 147
and Adkins .. i r,
Wittich, E. . IIIIIIIIIIIIIzil
Woodbine? flora 44
Woods, H. 1M, 227, 231
Yabe. H. igg
Zacatecas. Mexico go
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