GEOLOGY OF THE PROVINCE
OF CAMAGUEY, CUBA, WITH
REVISIONAL STUDIES IN
RUDIST PALEONTOLOGY

TER VERKRIJGING VAN DEN GRAAD VAN
DOCTOR IN DE WIS- EN NATUURKUNDE
AAN DE RIJKS-UNIVERSITEIT TE UTRECHT,
OP GEZAG VAN DEN RECTOR MAGNIFICUS
Dr. W. E. RINGER, HOOGLEERAAR IN DE
FACULTEIT DER GENEESKUNDE, VOLGENS
BESLUIT VAN DEN SENAAT DER UNIVER-
SITEIT TEGEN DE BEDENKINGEN VAN DE
FACULTEIT DER WIS- EN NATUURKUNDE
TE VERDEDIGEN OP MAANDAG 7 JUNI 1937,
DES NAMIDDAGS TE 4 UUR

DEZE DISSERTATIE VERSCHIJNT TEVENS ALS No. 14 VAN DE PHYSIOGRAPHISCH-
GEOLOGISCHE REEKS DER GKOGRAPHISCHK EN GEOLOGISCHE MEDEDEELINGEN

Aan het einde van mijn academische studiën, is het
mij een behoefte U, Hoogleeraren in de Faculteit der
Wis- en Natuurkunde, van wie ik mijn wetenschappe-
lijke opleiding mocht ontvangen, mijn dank te betuigen.
Dit geldt in de eerste plaats mijn Promotor, Prof
Dr. L. M. R. Rutten.

Gedurende mijn studententijd verwierf ik vele
vrienden. Hen voor hun vriendschap te bedanken zou
onjuist zijn. Deze jaren zijn er echter onvergetelijk
door geworden.

General ; Pétrographie descriptions ; Age of
the Tuff Scries : I Provincial Limestones,
II Ammonite Limestones, III Geologically.

Loma Yucatan Limestones ; Camajan breccia's
Barrettia-beds sensu stricto ; Age of the
Mabana Formation.

PART II : REVISIONAL STUDIES IN RUDIST PALEON-
TOLOGY. MAINLY BASED UPON COLLEC-
TIONS FROM CUBA.

Ichthyosarcolitinae ; Trechmannellinae ; Rous-
seliinae ; Antillocaprininae ; Genera of doubtful
position (Immanitas, Lithocalamus).

Check list of American Caprininae ; Discussion
of Caprininae ; Check list of American
„Caprotininaequot; and Polyconitinae ; Plagiop-
tychinae.

In 1933 an expedition of the Utrecht University under the leadership
of Prof. Dr. L. M. R. Rutten, set out to explore the geology of parts of
the Isle of Cuba. The other members of this expedition were Mrs. Dr.
C. J. Rutten-Pekelharing, Miss A. Röntgen, Dr. M. G. Rutten, Dr.
A. A. Thiadens, Dr. L. \V. J. Vermunt, and the author.

From April 22th to May 4th, we worked in the Province of Camaguey
situated in the Eastern half of the Island. Our central camp was pitched
m the domam of the Granja Escuela, just East of the town of Camaguey
or Puerto Pnncipe, and from this base most of the work was done. After-
wards two of us surveyed the neighbourhood of Central Senado, enjoying
hospitality there. The weather was fair, the country little accidentated and
the roads tolerably good. So, most of the work was done by car, and large
distances could be covered in one day. This was made possible, moreover,
by the scarcity of outcrops, and by the extensiveness of the areas often
covered by a single formation. And so, each day we set out in parties of
two, each perpetually on the look-out on either side of the car, letting out
loud cries of „pare, parequot;, whenever an outcrop was sighted.

For general orientation we used the military maps on a one-inch-a-mile
scale, which were put at our disposal through courtesy of the Cuban Govern-
ment. These maps, however, were insufficiently accurate in detail, so that
we had to do our own mapping. This was done by taking direction with
a geological hand-compass, while for the distances we relied upon the
speedometers of the cars, checking their accurateness from time to time
with the milestones of the Carretera Central. Generally they gave about
40 meters to much to a kilometer. If on foot, we counted our paces. The
distances got in this way are liable to an error of about the same order
of magnitude. A similar error may exist in the compass-readings. As errors
of this magnitude have little effect upon the aspect of the geological map,
no corrections have been made for them, even though the error of the
speedometer is systematical.

From the first it has been our intention to give our work the nature
of a preliminary survey. Several factors combined to give it this character.
First of all next to nothing was known of the geology of this region before
our stay, and the few data available often were conspicuously incorrect.
Thus a general survey promised to be much more valuable than the detailed
mapping of a small area. This, moreover, would have been impossible
without a reliable topographical map, and then, any ambition of this kind
would at once have been squashed by the scarcity of outcrops. Upon the

enclosed map the surveyed courses have been indicated by dotted lines,
with a full-drawn line for the Carretera Central. In this way the experienced
reader will at once be able to judge, what is based upon fact, and what
mere interpretation. Blank spaces have been left, where extrapolation would
have been too hazardous, and boundaries have been drawn only, where
there was sufficient probability.

There is one source of error, special to this region, on which emphasis
must be laid from the first. The field-observation was made especially
difficult by the deceptive similarity of the rocks of different formations.
Rocks that in the field had been confidently put down to the Tuff Series,
often appeared in the laboratory to be uralitized diorite-porphyrites, quartz-
epidote rock, or glass-tuffs of the Upper Cretaceous, which makes all the
difference between Dioritic rocks, Habana-formation and Tuff Series. In
this way it is possible, that, for instance, the boundary between Tuff Series
and Habana formation may be wrong a few kilometers, even on the very
courses surveyed. So, the next surveyor of this region will have to pay
special attention to this, and, if no laboratory work can be done along
with the field-work, extensive sampling will be the only way out of this
difficulty.

All notes of field-observations and all the material collected in the
Province of Camaguey by our expedition, were turned over to the writer,
who worked out the data in this paper. Notes and material have been dep-
osited in the Mineralogical Geological Institute of Utrecht.

We may round up with a few explanatory remarks about the dualistic
nature of this work, as expressed by the double title. Rudists are not the
only fossils found in this region, but they make up the bulk of our paleon-
tological collections, and had the author's special interest. Even so it seemed
more useful to treat a few groups of this family in a more extensive way,
submitting them and their allies to a submonographical study. Of these
groups the material of the other regions surveyed, which had already been
treated in paleontological papers by my colleagues, was kindly turned over
to me for further study. In this way, however, the second part of this work
did not follow naturally as the paleontological part of the geologic study
on the Camaguey region, but developed as a more or less independent
work, which may explain, why it is separated under a title of its own.

As I am indebted to many, both in Cuba and in Holland for their help
and kindness, I should like to express my gratitude here.

In the first place I wish to express my indebtedness and sincere thanks
to Prof. Dr. L. M. R. Rutten, whose matchless leadership of this expedition
whose large experience in field-work and whose ever-ready advice, support
and personal interest, when difficulties of any kind had to be tackled, have
been of inestimable help to me.

To Mrs. Dr. C. J. Rutten-Pekelharing, whose experience of tropical
life helped us over many a difficulty of every-day life.

To my colleagues M. G. Rutten, A. A. Thiadens and L. W. J. Ver-
munt for their excellent comradeship and mutual understanding.

The „Molengraaf-Fondsquot; and the „Bataafsche Petroleum Maat-
scHAPPijquot; for their pecuniary aid to our expedition.

The Cuban Government and the Sociedad Geografica de Cuba,
whose assistance was always at our disposal.

Ingenior Felix Malberti who was the first to introduce us to the
lures and beauties of the Cuban landscape.

Dr. Tschopp, Mr. R. H. Palmer and Mr. Lopez-Trigo who increased
our collections with valuable material. The long discussions with Dr
Tschopp on the geological problems of Cuba have been of great assistance

to our work To him also we own our knowledge of several important
nnd-spots of fossils.nbsp;^

Senor R Casal y Marqueti, for granting us permission to pitch our
camp upon the domain of the Granja Escuela, and to the owners of the
L^entral benado for their hospitality.

Prof. Dr. Ir. J. I. J. M. Schmutzer, whose advice on petrographical
problems was always at my disposition.

Mr. W. van Tongeren, who did some chemical and spectographical
analyses for me.nbsp;^

Prof. Dr. F. Trauth of Vienna and Prof Dr. E. Jaworski of Bonn,
who undertook the study of the Camajan Aptychi and Ammonites.

Mr. L. A. H. Bouwman, whose able pen drew the figures PI 5 ff 7
8 and of p. 123, textf. 2.nbsp;o • gt; • ,

Mr. J. H. M. van Dijk, who executed with great care and tireless
energy all other drawings, all photographic illustrations and the map

Prof Gerth of the Geological Institute of Amsterdam, Prof E. Broili
of Munich, Prof W. O. Dietrich and Prof F. Klinghardt of Berlin
and Mr. L. R. Cox of the British Museum, for lending me Rudist
material for comparison with our collections.

During our stay on Cuba at every turn we met with the greatest kindness
and friendliness from the side of the Cuban, poor or rich. We can only
hope to be able to pass on the debt of their hospitality.

As in the Province of Santa Clara i), there is in Camaguey Province a
great contrast between the Northern and the Southern half, a contrast both
geological and tectonical. Serpentine crops out in a large area in the North,
while in the South it has not been found. The post-cretaceous folding^
which is comparatively gentle in the South, has been very strong in the
Northern parts, where vertical limestone-breccia's have been thrust into
the Camajan-limestones.

Upon the map of De Castro-Salterain (1919, Bol. de Minas) a patch
of „Paleozoicoquot; is indicated to the Southeast of Nuevitas, at the boundary
between Camaguey and Oriente. Our survey did not reach as far as that.
On Lewis's map it has been omitted.

The oldest rocks exposed in the surveyed area are the Aptychi-lAmz-
stones of the Sierra de Camajan, thin-bedded, veined, chert-bearing lime-
stones, which contain Aptjchi and Ammonites. This formation belongs to
the Lower Cretaceous as was proved by the ammonites.

After a time volcanic activity set in, and the beds of the-Tuff Series
were deposited. They consist mainly of porphyrites, diabase-porphyrites,
porphyrite-lavas and coarse porphyrite breccia's. Of great interest is the
occasional occurrence of primary amphibole in these porphyrites. At M 846
a probably intercalated limestone was found, which contains /Mj/-remains,
probably belonging to the Sahinia sp. described by Thiadens from Southern
Santa Clara (cf. p. 9). We take this limestone to be of Albian age. It is
clear, that parts of the thick Tuff Series may be older or younger than this;
indeed it is thought to be of Neocomian to Coniacian age (cf. pp. 10—13)!

These strata were afterwards intruded by Peridotite, which, in its
mm, was intruded by a rest-magma of Gabbro's and Gabbroid' Rocks.
Thereupon an intrusion of Dioritic Rocks followed, which metamorphosed

They will be bnefly referred to by the names of their authors, or by the name of he Province.

the TufF Series. Diabasic rocks near Cromo are thought to be an intrusion
of Dioritic origin into the Serpentine.

The first orogenesis, which folded the Tuff Series beds may be thought
to have occurred at about the same time as the intrusion of these magmatic
rocks, or shortly afterwards.

After a period of denudation, the Habana-formation was deposited,
which is of Maestrichtian and probably partly of Campanian age, and
disconformably overlies the older formations mentioned, of which 'frag-
ments are contained in its conglomeratic members. The lithological aspect
of this formation is highly variable. Thick masses of glass-tuffs and glass-
tuffites show, that the volcanic activity had by no means ceased at this
time. Apparently there is an increase of volcanic activity towards the East;
while in Pinar del Rio no vestiges of this activity were found, and while
m Santa Clara they play a not unimportant role, they make up the bulk of
the formation m Camaguey Province. No intrusive rocks have been found
in this formation. The tuffs and tuffites seem to form the base of the form-
ation in most cases. Further constituants are limestones, tuffaceous lime-
stones, sandy hmestones, recrystallized and ^//^Z/jMimestones and Lamelli-
branchiata-httccWs. At the North, in the Sierra de Camajan, the formation
consists of breccia's, limestone-breccia's and marls, which contain Rudist-
fragments and Orhitoids. Detritic Tuff Series and Diorite material is of frequent
occurrence in the sandy limestones and in the breccia's, while in the North
at one locality a breccia was found to contain fragments of Serpentine.

A new orogenesis and, after that, a period of denudation followed the
deposition of the Upper Cretaceous beds, and was followed by the deposition
of the Eocene strata. Volcanic activity had come to a stop by this time.
The oldest member of this formation seems to be the Cubitas limestone
which may be older than the Upper Eocene.

Typical Upper Eocene has been found to the North of the Cubitas
Mountains. Upper Eocene is also exposed in the Southern part of Camaguey.
The Sierra de Maraguan is also thought to belong to the Upper Eoccnej
although no Lepidocyclime were found there. Detritic material of the Diorite
is more frequent still in the Eocene than in the Habana Formation, showing,
that more diorite had become exposed by this time. Serpentine fragments
were found in the Cubitas Limestone, and detritic Rudist and Orbitoid
fragments in the Eocene area Northwest of Florida.

A renewed folding disturbed these beds. Both in the North and South
this orogenesis is much weaker than that which followed the close of the
Cretaceous. The force of the Pre Maestrichtian folding could not be as-
certained, in the South through lack of sufficient tectonical data, owing
to the nature of the TufF Series, in the North because of the great force
of the Post Maestrichtian orogenesis.

Oligocene has been recorded from the neighbourhood of Nuevitas by
G. Bruscantini (1929, Bol. de Minas, Habana, 14, pp. 55—63); it is

insufficiently established. The Echinoidea of the Loma Calisto near Nuevitas
described as Lower Oligocene by SAnchez and Lambert, are accompanied
by Discocyclina, and belong therefore to the Upper Eocene. The Southern
Oligocene mapped by Lewis seems to be based on phantasy. It does
certainly not occur as far to the North as has been mapped by that author.

As will have been seen, the geologic history of this Province is virtually
the same as in the other Provinces, as described by Rutten, Thiadens
and Vermunt. There is no evidence here that the Serpentine is really
younger than the Tuff Series, and this was concluded from analogy with
the other Provinces. Everything else has been proved by independent
arguments.

This formation is exposed in the Sierra de Camajan, which consists
entirely of these limestones, with wedged-in scales of Habana-formation.
It must be stated, that the proportion between the extent of Aptychi-Vimamp;ston^
and that of the Habana-formation is not known. In the map we coloured
the Camajan Mountains mainly blue, with but a few patches of Habana-
formation. It is quite possible, that this will have to be reversed, and that
the bulk of the outcorps belongs to the Upper Cretaceous.

The Aptychi-lAmt^tont^ are rather monotonous and lithologically
much the same as those of Northern Santa Clara and of Pinar del Rio
Province. They are buff to greyish blue, fine-grained, compact and generally
thm-bedded ; they are mostly full of Radiolana and a certain amount of
asphalt seems to be always present. Other members are cherts and radio-
larites. Several asphalt pits are known to the population. From one such
a pit (A 571) an extremely thin-bedded limestone was collected, with asphalt
along the bedding. It may be noted, that similar fragments were found in
a Habana-Formation breccia, sampled 40' down in another nearby asphalt
pit (A 568).nbsp;^ ^

The formation has been intensively folded by the Post Maestrichtian and
Pre Upper Eocene orogenesis, for the Upper Cretaceous breccia's are just as
intensively folded as the ^/^(r/;;-Limestones, whereas the nearby Cubitas
Eocene, is but little disturbed. No definite structure could be observed,
and strikes and dips run in all sorts of directions. No angular disconformity
could be observed between the v^^^'lt;rZ»/-Limestones and the younger brec-
cia's. Nevertheless as will be seen in the tectonical chapter, the older form-
ation must have been actively disturbed by the Pre Maestrichtian orogenesis
as well.

Age of the Aptychi-Limestones: An undeterminable Laffiellaptjcbus from
loc. A 569 has been described by Prof. F. Trauth (1936, Proc. K. Ak.
Wet. Amsterdam, 39, 1, pp. 74, 75). It was considered to be of the same
age as the LMwellaptychi from Pinar del Rio Province, i. c. of Neocomian
and probably of Lower Neocomian age.

More detailed information was gained from the determination of the
Ammonites themselves, which has been undertaken by Prof. E. Jaworski
of Bonn. A publication on these and the Ammonites of the other Provinces
will be published soon by him. Prof Jaworski has been kind enough to

write me the results of this examination anticipatorily to his publication :
We herewith translate the contents of his letter:

Loc. A 562 : „Toxocerasquot; sp. indet., showing, that besides Crioceras
pulcherrimus d'Orb. (found in Northern Santa Clara, loc. H 488/9, near
Corazon de Jesus) still other evolute Ammonites are represented in this
formation.

Loc. A 565 : Crioceras sp. indet. B. Both localities (A 562, 565) probably
of the same age as the loc. H 488/9 in Northern Santa Clara, i. e. of the
Hauterivian or Barremian, certainly not older than Hauterivian.

Neocomites in the Valanginian of Europe, with „vereinzelte Nach-
züglerquot; in the Hauterivian. In Argentine Neoc. praeneocomiensis Burckh. and
Neoc. densestriatus Burckh., already in the Upper Tithonian. The same
species according to Burckhardt in the Lowermost Berriasian. The age
thus would be Tithonian-Valanginian. The occurrence of Oppelia seems to
disagree with this, for the forms of the nisoides-giowp indicate Aptian age.
Forms comparable to the Cuban fossil are not known from the Lower
Cretaceous. So there are two possibilities : a) Oppeliae related to ?}isoides
occur in Cuba already in the Lower Cretaceous, or b) Neocomites, in Cuba,
reaches up into the Aptian. The latter possibility, however, is most im-
probable.

We may add to this, that the loc. L 656 lies just West of A 565 ; it is
situated upon the end of the other course, indicated on the map. A 565
was found to be PHauterivian-Barremian, and thus just intermediate between
Valanginian and Aptian.

Everything considered the age of the formation may be put as Lower
Neocomian, possibly partly Upper Neocomian.

The Tuff Series occurs only in the Southern half of the Province,
where, with the intrusive Dioritic rocks, it forms the basement. Its lithology
is rather monotonous. We mostly found porphyrites, porphyrite-lavas, and
porphyrite-breccias ; the latter sometimes extremely coarse, and thus difficult
to sample. Diabases are rare. Most of the glass- or crystal-tuffs regarded
in the field to belong to this formation, appeared in the laboratory to belong
to the Upper Cretaceous. This was shown by the occurrence of quartz,
or by their occurrence below the Rudist Limestones, sometimes by both
at the same time. A few other tuffs, on the other hand, show signs of meta-
morphism caused by the diorite intrusion. At V441, for instance, an
epidotized crystal-tuff has been found, which is moreover pervaded by a
quartz-epidote veinlet. This tuff clearly belongs to the Tuff Series. The few
remaining tuffs, which offered no argument at all, leave us entirely in the dark.

as intercalated in the TufF Series. The first from locality M 846 is a coarse
conglomeratic limestone, with rounded-ofF fossils. Amongst these a canal-
bearing Rudist, with radially stretched marginal canals, and many polygonal
canals, which increase in diameter towards the interior. A septum is probably
present. The fossil thus would belong to the Caprinime, and it probably
is identical with the ,,Sabinia spr of Thiadens (1936, Proc. K. Ak. Wet.
Amsterdam, 39, 9, pp. 1140, 1141 ; textf 5(1)), which would mark an
Albian age (cf : Age of the TufF Series). The second sample, a marmorized
limestone from L 675, is pervaded by whisks of chlorite. One of these,
if seen in unpolarized light shows a distinct porphyritic texture. So here
we may have an intercalated limestone, injected by a subsequent porphyritic
intrusion.

For a description of the more common rocks, we may safely refer to
the theses of Rutten, Thiadens and Vermunt. Only a few aberrant rocks
will be briefly treated.

No distinction could be made between porphyrites and spilites in this
Province. The fresh porphyrites mostly bear more or less basic felspar,
whilst the albite-bearing porphyrites are mostly so rotten, that the acidity
of the felspar may as well have been secondary.

M 839 : augite-porphyrite : a porphyrite with numerous augite pheno-
crysts, and but a few entirely altered felspar phenocrysts. Amygdules arc
present, which have an opal-coating and a core of caldte. This sample is
curious because of the presence in one patch of numberless small idio-
morphic augites.

M 841 /2 : porphyrite-lava : f luidal texture distinct. Groundmass vitreous
with dendritic microliths of ore-minerals, which occasionally pervade the
felspar crystals, and with many small biotite plates, often arranged in parallel
groups. In this groundmass swim a large number of small felspar laths,
split up at both ends by protoclasis, sheaf-like. There are also larger pheno-
crysts of both augite (rare) and felspar (labrador), the latter often clotting
together, their oudines intact.

A curious set of porphyrites occurs at the road from Marti to Esperanza:
H 680 : amphibole porphyrite : a porphyrite with many inclusions of a more
ordinary type of porphyrite. This and the following samples are at variance
by the lightness of their groundmass under the microscope : the groundmass
of the ordinary porphyrites is mosdy darkish brown through the presence
of much more or less diffuse limonite, or other ore-microliths. There are
phenocrysts of zonal felspar and of calcitized hornblende. The latter are
ore-rimmed. Their amphibole-outline is unmistakable. The occurrence of
amphibole in the TufF Series is of great importance, because it is always
used to discern the presence of dioritic rocks. The following samples,
however, show clearly, that in these parts the amphibole-bearing porphyrites
arc just aberrant Tuff Series porphyrites.

H681 : olivine diabase porphyrite : felspar is present as very small
laths in the groundmass. The phenocrysts are: monoclinic pyroxene and
fresh olivine, with but little serpentinization along the cracks.

H 683 : augite-bearing amphibole porphyrite: twinned, zonal, and
sometimes zonally twinned labrador-bytownite felspar phenocrysts. Femic
phenocrysts of often twinned augite, of sometimes twinned amphibole and
of biotite (rare). The amphibole and biotite phenocrysts have ore-rims,
and the biotites have capricious outlines, showing their partial magmatic
resorption. Often an ore rim is found without its phenocryst, if the latter
has been secondarily altered.

H 684 : biotite-bearing augite-porphyrite: similar to the preceding
sample. Here the augites also may have a thin ore-rim. One amphibole
was found, which has a heavy ore-rim. The ore-rim bearing biotites again
give evidence of their magmatic corrosion by the capriciousness of their
outlines. The groundmass of this rock is darker, and thus transitional to
that of a more ordinary type.

H684^: a porphyrite of ordinary type: groundmass darker again,
vitreous, with limonitized ore-dendrites. Phenocrysts of zonal felspar and
of augite (rare). One or two ore-rimmed amphibole phenocrysts, however,
are still found. Patches of the groundmass are chloritized.

H 686 : augite porphyrite: No longer any amphibole present. Zonal
albite-oligoclase felspar and augite phenocrysts. The latter are ore-rimmed.
The felspars are often altered to zeolites. There are many apatite prisms,
pinkish to flesh-coloured and subpleochroitic.

And so it is seen, that the aberrant porphyrites of H 680—683 grade
into porphyrites of almost common type, showing, that the aberrant rocks
belong to this series and not to one of the other formations.

Another aberrant type of rock occurs at the coursc South of the Car-
retera Central at about H 722. We will have occasion to describe them,
when dealing with the Tuff-Diorite contact.

1. Caprinid or Provincial Limestone. This limestone is best exposed
in the South of Santa Clara Province (cf Thiadens, 1936, Proc K Ak
Wet. Amsterdam, 39, 9, pp. 1132-1141). The following fossils have been
encountered: Coalconiana ramsa, Caprimdoidea perfecta, Caprimdoidea sp.,
,Mbima sp:\ ?Tepeyacia corrugata. Coalcomana ramosa is also found • a) at
Soyatl^ de Adentro, Jalisco, h) Coalcomdn, Michoacdn, c) Escamela Lime-
stone Orizaba, Vera Cruz, all in Mcxico. Caprimdoidea occurs at a) Soyatlan
de Adentro, Jalisco, e) (C. whitei) Choy Cave. Taninul Limestone, Sierra
hi Abra, San Luis Potosf, both in Mexico. Further probably also c) (C
fehxi, «/ etc.) in the Escamela Limestone and fj (?C. anguis) in the Texan
Edwards Lime^one. Tepejacia was found c) in the Escamcla Limestone
and d) m the Tepeyac Mts., Puebla, Mexico.

We may briefly enumerate the different species, that constitute the
fauna at these localities :

a) Soyatlan de Adentro : Nerinea, Actaeonella, Apricardia chave^i, Monopleura
sala^ari, Chaperia sodalis, Barjconites multilineatus, Planocaprina trapet(pides,
Coalcomana ramosa, Caprinuloidea several sp.

The fauna was thought to be Cenomanian from analogy with
Coalcoman and the Escamela Limestone.
h) Coalcoman : Chondrodonta aff. mimsoni, Nerinea cf. Jorojuliensis, castilloi,
Serpula sp., Petalodontia felixi, calamitijormis, Coalco??iana ramosa.

c)nbsp;Escamela Limestone: Nuhecularia sp., Glohigerina crefacea, Bulimina sp.,
Orhitolina aff. lenticularis-, Triploporella fraasi, Neomeris (Heroiwalina)
cretacea ; Nerinea cf. forojuliensis, harcenai, goodhalli, Actaeonella ; Chondro-
donta aff. mmsoni, Pecten sp.; Apricardia chave^i, Petalodontia sp., Himerae-
htes sp., Tepejacia corrugata, Planocaprina sp. (Caprina cf adversa), Coal-
comana ramosa, ?Caprinuloidea (felixi, lenki, etc.), „Radiolites sp.quot; etc.

This and the preceding fauna were thought by Douvillé and
Boehm to belong to the Cenomanian on account of the similarity of
the Caprinids to forms of Sicily and the Italian Alps, then thought to
belong to the Lower Cenomanian. Both European fauna's, however
have since been put into the Lower Turonian. And then, it will be
contended on pp. 144 seq., that the American Caprinids are fundamentally
different from the European forms. The entire argument thus fails, and
for correlation we must needs turn to comparable American faunae.

d)nbsp;Tepeyac Mountains : Tepejacia corrugata. Thought to be Turonian, of
the same age as limestones near Huescalapa, Jalisco, Mexico, on purely
lithogical grounds. The fauna of Huescalapa consists of three species
of „Radiolitesquot; wliich I consider to belong to Eoradiolites, a „Sphaeru-
litesquot;, Requienia and Bajleoidea clivi. Requienia is not Turonian, and
Eoradiolites occurs frequently in older strata, so that it is not even clear,
why the Huescalapa fauna should be Turonian (cf. also Burckhardt,'
1930, Mém. Soc. Pal. Suisse 49/50, pp. 208—209).

e)nbsp;Choy Cave: Chondrodonta cfr. munsoni, „Capfmula spr, Caprinuloidea
whitei, Eoradiolites aff. quadratus.

f)nbsp;From the Edwards Limestone we may cite: Chondrodonta munsoni,
„Caprinulaquot; (? Caprinuloidea) anguis, Eoradiolites quadratus, angustus, david-
soni, etc.

Apparently all these faunae are intimately related and so we may parall-
elize them all to the Edwards and Taninul (Choy Cave) divisions, which
had already been correlated to one another e.g. by J. M. Muir (1936, Geology
of the Tampico Region, Mexico). The Taninul and Edwards division have
been correlated to the European Albian (top of the Middle Albian), and
we may therefore regard the other faunae mentioned and the Provincial
Limestone of Cuba to be Upper Middle Albian.

Two arguments may be brought up against this parallelization. First,
the different forms may have persisted for some time, and so they might
occur also in either older or younger strata. Without further argument,
however, there is little reason for such suppositions. The second argument
regards the correlation of the Edwards to the Mddle Albian. If we count
up the different Radiolitinae, regarded as Pre Cenomanian, we find, that a
surprising number of them (about half) hails from the Edwards Limestone.
So an Upper Albian age or even Lowermost Cenomanian might be thought
more probable. This objection, however, is not conclusive, as but litde
is known about the European Pre Cenomanian Rudists.

All considered we .may assume an Albian (Edwards) age for the Pro-
vincial Limestones. A neritic zone, at that time, extended from Texas, over
El Abra Sierra, Escamela, Coalcoman, Soyatlan de Adentro, Tepeyac down
to Cuba.

IL ^//?/;/ö«//^-Limestones. At two localities in Northern Santa Clara
Ammomte-ht^im^ limestones have been found (cf. M. G. Rutten, pp. 7
36), which have been regarded as intercalated in the Tuff Series. Prof E'
Jaworski, who undertook their identification, considers them to be of
Turoman to Coniacian age. It is a curious thing, that from Chiapas an
Ammomte-ï'x\xvi'^ of about the same age has been recorded by F. K. G
Muellerried, as intercalated in the ^^rr^/Z/^-limestones (cf p. 26). The
two faunae have one genus in common, to wit Pachydiscus. Now in Cuba
there is no doubt, but that the .S^rr^/Z/^-limestones lie disconformably over
the Tuff Series. So, if the Ammonite-faunae in Mexico and Cuba are really
of the same age, and if the Ammonite-bearing strata in Cuba are really
intercalated m the Tuff Series, then we must assume the existence of a
tectomcal complication in the Chiapas profile. We may note, that, as will
be seen, a Maestrichtian age need scarcely be doubted for the Barrettia-
hmestones. This too points to a tectonical complication in Chiapas.
, ij^- Geologically, the following may be said. M. G. Rutten regarded
the TufF Series to be partly contemporaneous with part of the Aptychi
Limestones. Vermunt, however, showed, that the Tuff Series in Pinar del
Rio Province follows directly above the Aptychi Limestones, and that
consequendy they are younger, which is in accordance with the faunal
correlations of Aptychi Limestones and Tuff Series. So in Northern Santa
Clara we must assume, that the limit between Aptychi Limestones and Tuff
Series is less sharp than in Pinar del Rio Province,' or that still more tccton-
ical complications exist in Northern Santa Clara, than have already been
mapped by Rutten.nbsp;^

are frequent in the lower parts of the Tuff Series, and become less frequent
m the younger parts of that formadon.nbsp;frequent

We are accordingly led to the following conclusions. At some time
unknown, after the deposition of the Lower Neocomian Aptychi^Limcstoncs,

volcanic activity set in, changing entirely the aspect of the depositions.
This activity persisted with undiminishing force up to the beginning of
the Senonian. After that intrusion and folding took place, somewhere
between the Coniacian and the Upper Campanian.

A Serpentine-Tuff Series contact may be present at one place only,
i. e. South of the Carretera Central near H 647. It has not been visited by us!

Contacts between TuflF Series and Diorite are frequent. Several contact
phenomena have been observed.

1.nbsp;The intrusive nature of the diorite is obvious from the map. An augite-
porphyrite sampled at M821, appeared under the microscope, to be
intruded by a minute aplitic veinlet.

2.nbsp;At L 722^, an epidotized quartz diorite porphyrite was sampled, which
contains distinct inclusions of Tuff Series porphyrite groundmass

3.nbsp;Metamorphism of the rocks of the Tuff Series, chiefly uralitization, and
epidotization is of frequent occurrence. Some examples of this will be
given below.

4.nbsp;„Marginal fadesquot; of the Diorite. It must be stated, that, to judge from
our samples, normal diorite is rare in this Province, and that most of
the samples show a „marginal fadesquot; in one way or another. Even the
typical „\Vollsackquot;-diorite near Sibanicu proved in the slide to be
mostly porphyritic with microgranophyric groundmass.

In the following we give a few examples of typical contacts.
L 709—711, South of Florida, going from the Northeast to the South-
west:

L 709 a quartz amphibole diorite porphyrite; porphyritic texture but
faintly indicated.

L710quot; an augite-porphyrite brecda; showing uralization on a small
scale. Small uralite crystals have been formed along cracks in the rock, or
they form small clusters round some of the plagioclase and augite pheno-
crysts. Some of the augite phenocrysts are partly uralitized along the cleavage.

L710^ a quartz-amphibole diorite porphyrite, partly epidotized;
porphyritic texture more distinct than in L709.

L710'^ augite porphyrite brecda ; strongly uralitized ; groundmass full
of fibrous uralite; augite phenocrysts uralitized at the outer rim and along
the cleavage.

L 711 quartz amphibole diorite porphyrite ; most typically porphyritic
texture; quartz phenocrysts much corroded, with capricious outlines;
amphibole phenocrysts with ore-rim; a little epidote present.

L7ir a problematical rock, which probably is of mixed origin: it
contains many porphyrite fragments, some clearly belonging to the Tuff
Series, others with a more diorite-porphyrite like aspect. The whole much

uralitized addition to this, one finds many quartz crystals and much
epidote. This rock is either a volcanic breccia of the Dioritic magma, or a
Tuff Series porphyrite breccia, influenced by quartz-epidote emanations.
In the latter case, aU porphyrite fragments must be reckoned to the Tuff
Series, as well they may, for some Tuff Series porphyrites are very similar
in texture to porphyrites of the Diorite.

_ L711^ a porphyrite with much fibrous amphibole, which, on closer
inspection, appears to have the outUne of augite phenocrysts. The cleavage
also IS not parallel to the outline. Apparently a porphyrite of the Tuff Series
with the augite phenocrysts entirely uralitized.

A^rious contact is present near H 722, South of the Carretera Central
From West to East we get:

rt7r t ? ? ^quot;JPhiboles, but wich have a much too oblique extinction.
Ihe rock is calcitized and chloritized in patches.

thini^lJff A/f' phenocrysts of greenish monoclinic pyroxene are the only
thmg left of the origmal rock. The rest is a mass of curiously intert^vined

porphyritic malchite ; fine-grained dioritic rock, rich in primary
often idiomorphic, poikilidc amphibole. In addidon to this large Zno'

needles, and large greenish monoclinic pyroxene. There is a noticeable
amount of secondary minerals, such as epidote and chlorite in the dyke rock.

H 730 augite porphyrite. Intersertal groundmass of felspar with chlorite.
Large phenocrysts of often entirely calcitized felspar, and of partly uralitized
monoclinic pyroxene. Amygdules filled with calcite, chlorite or both.

L749 lamprophyric Diorite dyke rock. Fine to coarse grained with
numerous small green pyroxene crystals. Large pyroxene phenocrysts with
greenish outer rim. These rims with a slightly different extinction. Some
of the pyroxenes have sets of lineal ore-inclusions, intersecting at an angle
of 54° in one case and of 66° in another. In the latter, a twin with parallel
cleavage, these inclusion lines intersect the cleavage at different andes •
55, 11° and 71°.nbsp;amp;nbsp;5 •

L751 a Tuff Series porphyrite without metamorphism. Zonal felspar
phenoctysts, with reiterated zonation, incomplete, or halved through proto-
clasis Rare femic constituents: augite and biotite. Groundmass zeolitized.
ization ^^^^^^ amphibole diorite, with microgranophyric restcrystall-

L 752 chloritized diabase porphyrite; zeolite amygdules with a chlorite
coating.

Other typical contact rocks of the Tuff Series, all sampled near the
Diorite, are :

H 652 and 662 intersertal diabase porphyrites, much uralitized and
epidotized, with nests of secondary amphibole, epidote, quartz and chalco-
pyrite, and with deposition of epidote and zeolite along the joints.

V 522 a porphyrite with the pyroxene phenocrysts entirely uralitized
but still retaining their characteristic outline. The amphibole-cleavage is
not parallel to the oudine. The groundmass also is strongly uralitized :
full of small uralite needles and fibres. A curious feature of this rock is the
presence of small biotites in nests or as frequent inclusions in the uralitized
pyroxene phenocrysts.

The Serpentine covers an enormous area in the Northern half of the
Province. This area extends about 50 km from WNW. to ESE., and 20 km
across, interrupted only by Gabbro masses, the diabase intrusion near
Cromo, the Camajan Sierra and the Loma Yucatdn. Most of this area is
level country, covered by a crust of Serpentine residuals. „Cana»-palms
hard-leafed scrubs and meagre grass eke out a precarious living from the
solid soil. There is plenty of rain in the right season, but is does them but
little good, for each squall merely inundates the country, and the water
runs off along the surface. Small wonder, that one may go for miles.

without encountering a living soul, or a single dweUing to disturb the
magnificent wildness of this savannah.

The lithology of the Serpentine itself is very monotonous. Sometimes
a certain amount of bastite or of rhombic pyroxene is found, marking a
transition towards rocks of harzburgitic origin (L 647, H 647). The following
secondary rocks have been sampled: L 631^, a block of greenish opal, with
whisks of serpentine and magnesite ; quart2-rock (L 645quot;), occasionally
with chromite (L 645^) ; chalcedone (L651, M861); other silica-relicts
(L 660, A 537); and A 577, a sponge-like carbonate rock.

In the other provinces, and especially in Northern Santa Clara, many
inclusions of different kinds have been found in the Serpentine. In Camaguey
Province we only met with two inclusions at the localities L 657 and L 658,
just East of the town. Both are large masses of many hundreds of cubic
meters, the first of zoisite-amphibole-albite-schist (L657), the second of
quartz-zoisite-chlorite-schist (L658). Both are fine-grained.

A more gentle, scrubby vegetation indicates the presence of Gabbro.
There is more variation here : from ordinary gabbro to olivine-gabbro
(M 896) and troktolites (L 645^, L 65F, A 538, A 539). The cleavage of the
gabbro-diaUage is often distorted by subsequent orogeneric movements
It may be noted here that these have also imprinted themselves upon one
serpentine sample (L648quot;), which is slightly schistose.

The gabbros are much altered, with zeolirized felspar, much prehnite
or sometimes Ptalc (L 636^). They are further pervaded by prehnite veinlets,
which contain a certain amount of zoisite and epidote. Some gabbro's have
been actinolitized : for instance A 575, a much altered rock, with large
amounts of prehnite and small acrinolite needles, and with a little uralite.
L 649 IS an almost entirely actinolitized gabbro, with large secondary crystals
of this mineral. The felspar of the gabbros mostiy is labrador-bytownite,
but andesine m one case: L636^ this is the rock with Ptalc instead of
prehmte. A most curious rock is L 648, sampled as a dyke in serpentine :
It is a saussuritized garnet-bearing gabbro. At L 645 the gabbro is pervaded
by dykes of gabbroid anorthosite, with small amounts of diallage and
veinlets of prehnite with zoisite and epidote.

The troktolites are most typical, and consist of labrador-bytownite
and olivine. A small amount of diallage is found in L 645'. The serpentin-
ization of the olivine has cracked the surrounding felspar. These cracks
are radially arranged, and those caused by the serpentinization of one
olivine intersect those caused by the next one. In sample A 538 the ser-
pentine is even pressed into some of these cracks. In the olivinUabbro,
both felspar and diallage have been cracked up in this way

It may be noted, that the Gabbro occurs also as dykes in the Serpentine
m Northern Santa Clam (M. G. Rutten, p. 15) The anorthosites appquot;
are a further differentiation in the same direction.nbsp;^ ^

Age of the Serpentines and Gahhroid Rocks: It has already been stated
in the Introducdon, that no lower limit could be set to the age of the Ser-
pentines, in this Province. In Northern Santa Clara, however, it was proved
to be younger than the Tuff Series (M. G. Rutten, p. 13). Additional,
though a little less conclusive evidence was furnished in Pinar del Rio
Province (Vermunt, p. 18). We may safely adopt this view for our Pro-
vince. At two localities we found intrusions into the Serpentines which may
be reckoned to the Dioritic magma. Serpentine was moreover found as
pebbles in a breccia of the Habana Formation, sampled at locality A 568,
in the Camajan Sierra. Small fragments of Serpentine were also found in
the Cubitas Eocene at locality M868'. Everything considered, we may
regard the Serpentine with its Gabbroid differentiate, as younger than
the Tuff Series, and slightly older than the Diorite. As a consequence
it intruded during the Senonian.

In addition to the gabbroid intrusions already mentioned, we found
intrusive rocks at two localities:

Quarry near El Congreso (L 747, H 748). In this quarry white-coloured
dykes were sampled. They consist of larger hypidiomorphic to lenticular
albite-ohgoclase m a panallotriomorphic mass of albite-oligoclase and zeo-
lite, and are pervaded by veins and veinlets of prehnite and zeolites. Acces-
sory apatite was encountered in H 748iv. This sample has an important
amount of needles of undeterminable secondary minerals. The surrounding
rock was twice sampled. One sample (H 748^) is a saussuritized rock with
patches of serpentine. The other (H 748 V) is a saussuritized rock with large
crystals of secondary prehnite. It contains small aggregates of garnet, both
in the rock itself and in the prehnite crystals. The latter are aggregates of
more or less idiomorphic garnet.

Intrusion near Cromo. R. Allende (1929, Bol. de Minas, 14, pp. 11—22,
(manuscr. 1926)), in describing the mine of „Cromoquot;, mentions intrusions
in harzburgite of diabase, diorite granulite and muscovite granite. Hayes-
Spencer-Vaughan, in their report on the geology of Cuba (Second edition
of 1925, p. 96), only mention gabbroid intrusions here. Our party sampled
diabases at L 645quot;!. iv, v and L 646^ on the Nuevitas railway line in the
immediate vicinity of this mine. The samples of L 645 have a rather coarse
intersertal texture with partly uralitizcd, epidotized and chloritized pyro-
xene. Varying amounts of quartz are present as a rest-crystallization. The
rocks are rich in magnetite. L645iv is almost entirely uralitized, but the
amphibole sometimes has distinct pyroxene outiines. L646i is a coarse
quartz-amphibole-diabase, partiy chloritized. The texture of this rock is
most peculiar: the crystals show a spheroidal or better a centric arrangement,
caused by the centtic intergrowth of a few large amphibole and felspar
crystals, pegmatitic-like. I am inclined to reckon both categories to the

diontic rather than to the gabbroid magma. If this supposition is true then
we have here an argument indicating, that the Diorite is younger than the
Serpentine. It may be noted, that this relation was proved beyond reproach
m the Northern part of Santa Clara Province (M. G. Rutten pp 13 14)
There IS another phenomenon in Camaguey Province, which points the 'same
way. Of the 17 hydrothermal dioritic rocks sampled by our party, two were

Series contact, four in an isolated patch (L697n
L 745/6) which may or may not be near to a contact. All the others were
found m a belt along the Diorite-Serpentine boundary. On the whole I
get the impression of a distinct increase in „marginal fadesquot; of the Diorite
not only towards the Tuff Series contacts, but towards the Serpentine con-
tact as well. For a discussion of this, we would have to describe all the
Uioritic Rock samples, which would take us to far

All considered there is sufficient, though not conclusive, argument
m favour of the above stated relation between Diorite and Serpentine
concurring with the observations in Northern Santa Clara

Dioritic Rocks are subject to much more variation than the other
magmatic rocks described. It is possible, however, that this variation is

ot ruff Series and Serpentines. In the following I will not give a full des-
cription of all the varieties of Dioritic Rocks encountered i ƒ this Province
as much has already been written about the Diorites by my colleagues'
especially by Thiadens and Rutten. We will briefly enumerate the difS^

title varieties (H 666: a biotite-grano-diorite-pegmatite- L741- L 727. o
spheruhtic aphtic diorite-pegmatite).nbsp;' ^^' ^

amphibole-diorite-porphyrites, diorite-porphyrites, amphibole-diorite-por-
phyrites, and amphibole-porphyrites,

H 675 is an epidotized micro-pegmatitic quartz-amphibole-biotite por-
phyrite. Phenocrysts of labrador-bytownite, quartz, amphibole in a micro-
granophyric groundmass, centred towards the phenocrysts, and becoming
coarser towards them. There are clusters of magnetite with idiomorphic
amphibole, biotite, large augites and apatite.

M822 is a much altered and weathered porphyrite with the habitus
of a diorite-porphyrite, but with an augite phenocryst. There is, however,
also an unmistakable, though small quartz-phenocryst, with a glass inclusion.

In the field the diorite porphyrites are difficult to distinguish from
the Tuff Series porphyrites. L724, for instance, can only be recognized
as a diorite-porphyrite under the microscope.

c)nbsp;Leucocratic differentiates and dyke-rocks: mica-aplites, aplites albi-
tites and anorthosites (H 643).

The albitites mostly have a certain amount of muscovite, microcline
and, or orthoclase. H 655 is rich in pyrite. There is a large mass of them
at H 654—657 and another, already dealt with, at H 748, the latter in-
truding in the Serpentine.

The leucocratic rocks have been more severely influenced by subsequent
orogenetic movements than the other varieties.

d)nbsp;Melanocratic dyke-rocks: vintlites (V 491), malchitic vintlites (V 492),
malchites, porphyritic malchites, malchite-kersantites (V526), porphyritic
quartz-kersantites, kersantites (H661).

The kersantitic rocks are exposed near km 594 on the Carretera Central
East of Camaguey City (H658, 660, V526). H 658 is a porphyritic quartz-
kersantite; larger allotriomorphic untwinned albites in a panallotriomorphic
microcrystalline mass of smaller quartz and albite, with numerous small
idiomorphic biotites, and with orthoclase as a rest-crystallization. There
are also a few larger orthoclases and microcline. Other consdtuents: magne-
tite, apatite and garnet. H 660 is similar, but without garnet, more coarse-
grained. The biotites, smaller and larger, are very pale, sometimes almost
colourless. V 526, 526quot;!, sampled as inclusions in an aplite. Microscopical:
fine-grained mass of quartz and felspar with much amphibole and biotite
and very long apatite-needles. The surrounding rock is a granodiorite-aplite
with muscovite and pale biotite (V526I); V526quot; is similar, but coarser.

H 656 is a curious, green dyke-rock, cutdng through albitites. It consists
entirely of uralite and albite.

H 676 is a porphyritic malchite dyke cutting through a quartz-diorite-
aplite. Microscopical: a disdnct „Sahlbandquot; is observed. The large felspar
and quartz crystals of the aplite have been cut off sharply by this dyke.

To judge from this meagre evidence, the aplidc rocks must have been
younger than the kersantites, and the malchitic rocks younger than the
aplites.

e) Post-magmatic rocks: quartz-epidote-rock, quartz-epidote-uralite-
rock, epidote-chlorite-quartz-rock, quartz-sericite-rock and epidote-rock.

Inclusions in the Diorite. We have already mentioned the inclusion
of Tuff Series porphyrites in an epidotized quartz-diorite-porphyrite sampled
at locality L722a.nbsp;^ r jnbsp;r

Cataclastic phenomena: Around H 704—706 the diorite is distinctly
stretched, as can be observed in the field. Under the microscope, several
samples give evidence of subsequent stress: stretching, mylonitization etc.
At H 642 an almost gneissic aplite was sampled.

Alteration: postmagmatic emanations frequently have altered the Dio-
ritic Rocks to some extent. Epidotization is most frequent, chloritization
more rare and always coupled with epidotization. Often near to a rock

altered m this way, one of the above-mentioned hydrothermal dyke-rocks
was sampled.

^^^ ^f Diorite: Dioritic material frequentiy occurs in the rocks of the
Habana Formation. We have already stated our arguments for a younger
age of the Diorite than of the Serpentine. As a result the Dioritic intrusion
must have been Senonian, younger than the Peridotitic intrusion.

For the use of the word Habana Formation vide M. G. Rutten, p 20
The term itself was coined by R. H. Palmer.

t^acies : Camajan breccias without recognizable Rudists and the Barrettia-
beds s. str.

Loma Yucatan Limestones. Cropping out in two hills North of Cama-
guey City overlying the Serpentine. They consist of /«.rZ-breccia's and
^W/i/-reefs. No detritic material has been found in these limestones, and
not a single Orhitoid or Catnerina.

Durania curasavica (Martin) Mc. G. : L 634, V529.
Durania lope:(trigoi (^-Amzr)'. V

Vaccinites inaequicostatus macgillavryi (Palmer) : V 5'gt;9
Praeharrettia corralinbsp;V529.

The Camajan breccia's contain the same foraminiferal fauna as the
Barrettia-htd^ s. str. They contain the following detritic material: fragments
of asphalt-bearing Radiolaria-limtstonQ of the Neocomian, Glohotnmcana-
bearing limestone fragments of unknown origin, porphyrite-fragments of
the Tuff Series, Serpentine fragments (A 568) and plagioclase. At 562 in
a pit, two meters of marl were found overlying a silica-rock or chert with
chromite. The chromite was spectrographically analysed by Mr. W. v.
Tongeren. Besides Cr and Fe, it contains Mn (ca 3%), Ni, V (± 0,1
Mg, Ti and a trace of tungsten; cobalt could not be demonstrated.

A 564 is a little aberrant, as it is not a breccia, but a fine-grained lime-
stone or marl, showing, that there is not a fundamental difference between
this facies and the other, but that the difference is caused, by the nature
of the underlying sediments. This is of importance for the tectonical dis-
cussion on pp. 32, 33. A similar „Mountain faciesquot; was described from
Pinar del Rio Province. There also, the difference was put down to local
influences (cf Vermunt, p. 26). A facial difference between the Habana
Formation of North and South is also present in Santa Clara Province.

In Pinar del Rio Province no traces of volcanic activity during the
deposition of these beds have been observed. In Santa Clara Province, North
and South, however, there are beds of tuffs intercalated between the lime-
stones and clastic sediments. In Camaguey Province, the volcanic activity
seems yet to have been greater. Large packets of tuffs, crystal-tuffs and
Radiolaria-tn^its have been found mostly at the base of the formation but
also intercalated (H719 and L662quot;, both in the Arroyo Hondo syncline).

The tuffs are mostly light-coloured, greenish, fresh-looking, but also
darker often, sometimes not to be distinguished in the field from the tuffs
of the Tuff Series. This has been an important source of error in the field,
and much more sampling would have been done, had we but known of
this difficulty at the time. As it is, about four fifth of the sampled tuffs
appeared in the laboratory to belong not to the Tuff Series, but to the
Habana Formation.

These tuffs, mostly have a vitreous groundmass, light-coloured, fresh-
looking and perlitic. Some tuffs consist of glass only.

The crystal splinters of the crystal-tuffs are : mostly plagioclase, often
with quartz, and occasionally with biotite and amphibole (both in H 690a),

often a small amount of apatite is found and somedmes rounded-off grains
of epidote (H 690a). The tuffs quite often contain fragments of porphyrites
or porphyrite-groundmass from the Tuff Series, showing that they may
pardy be clastic. So some of the above-mendoned crystal-splinters possibly
may also be clasdc consdtuents, not proper to the magma itself A tuff
of Northern Santa Clara has been chemically analysed by W. van Tongeren.
(cf M. G. Rutten, p. 33, analysis nr. 17). Mr. van Tongeren has made
some spectrographical analyses for me of glass tuffs from Camaguey Province,
(L670, 677, H719) compared with a similar analysis of a glass-tuff from
Northern Santa Clara, sampled in the immediate vicinity of the analysed
glass-tuff (L36I). No important differences have been found. In addidon
to the elements that are always present, the following elements were found :
V, Cr, Mn, Sr, Ba, all (also the common elements such as K, Mg and Fe)
in comparable quanddes to those of the Santa Clara glass-tuff. As a result,
we may tentatively assume a similar chemical, i. e. about dioridc composidon
for these Habana Formation tuffs.

The clasdc sediments (sandstones, calcareous sandstones, conglomer-
ates, mffaceous and arkodc limestones) and limestones contain the following
detridc consdtuents : much plagioclase, often quartz, further amphibole,
pyroxene, biodte, porphyrite fragments of the Tuff Series, pegmatidc
fragments of the Diorite, and a silica relict probably of the Serpentine
(H 650). Brown hornblende was encountered in a calcareous sandstone
(L661) m the Arroyo Hondo syncline. This may indicate the presence of
amphibole-gabbros amongst the Gabbroid Rocks.

The limestones are rich in fossils, amongst which almost always Rjidist-
fragments, Vaughanina and Camerim dickersoni. Fossils like the two last-
named are the stratigrapher's friends : small, easily recognizable, and ever-
present.

The Rudists found at Arroyo Hondo close to the diorite, are often
silicificated, probably because of circulating solutions.

Faunal List (see: pp. 24, 25). In this following list we have included
the fossils and localides mentioned in the literature.

a)nbsp;A curious, strongly folded packet of limestone occurs near Redencion
(L 652-655). These limestones are fine-grained, darkish, and contain small
crystd-sp/wters of quartz and felspar, and small fragments of Tuff Series
porphyrites. The only fossils found are noncommittal: such as Radiolaria
and sponge-needles, and recrystallized fragments of tests of PLamellibranchi-
ata The tectonical and lithological aspect of these limestones, couplcd
with the presence of detritic quartzes and Tuff Series material, mark them
down as Habana Formation.

b)nbsp;In the collecdons given to us by Dr. Tschopp occur some Nerincids
from Ts 1007, 700 m S. of Aurora. If this is the Aurora in the Sierra de
Maraguan, we may assume, that the zone of Habana Formation which

stretches from Ingenio Grande to the Cantera Caballero (H 670, Ts 1098),
extends farther still, towards the Eastern end of the Maraguan Sierra.

The following literature is of purport to this question. Of each paper
the subject is given, and the conclusion to which the writer arrived :

1.nbsp;H. L. Hawkins, 1923, Geol. Mag., 60, pp. 215, 216 : Jamaican Echinids;
base of Upper Cretaceous to base of Senonian.

2.nbsp;C. T. Trechmann, 1923, Geol. Mag., 60, pp. 345, 346, Jamaican
Rudists etc. A Cardita cf. suhcomplanata, which species occurs in the
Indian Maestrichtian; Maestrichtian.

3.nbsp;H. L. Hawkins, 1924, Geol. Mag., 61, pp. 312—316 : Jamaican Echi-
nids ; Turonian or even Cenomanian.

4.nbsp;C. T. Trechmann, 1924, Geol. Mag., 61, pp. 393, 394: Jamaican
Rudists etc.; Campanian and or Maestrichtian. The occurrence of
Ostrea ari^ensis known from the Mexican Upper Senonian or
Maestrichtian is mentioned. The crab Carcineretes woolacotti, according
to Withers is the earliest crab in which the last pair of feet are known
to form swimming paddles.

5.nbsp;L. F. Spath, 1925, Geol. Mag., 62, pp. 31, 32 ; Jamaican Ammonites ;
One bed Campanian or even Maestrichtian, the other a little lower.

6.nbsp;H. Douville, 1927, B. S. g. F., (4) 27, pp. 49—56 : Cuban Rudists;
a whole time-scale is drawn on palaeontological evidence only; the
formation extends from the Turonian to the Maestrichtian f). Lambert
(p. 50) communicates, that comparable forms to one of Hawkins's
Echinids {Goniopygus) have been found in the Persian Campanian.

7.nbsp;C. T. Trechmann, 1927, Geol. Mag., 64, pp. 32, 64, 65 ; Jamaican
Cretaceous shales ; The Rudist-beds overlie the Campanian Ammonite-
bearing bed of Spath : Maestrichtian.

8.nbsp;J. Lambert, 1928, B. S. g. F., (4) 28, pp. 19—21 : Cuban Echinids:
Upper Cenomanian.

9.nbsp;N. E. Weisbord, 1934, Bull. Am. Pal., 20, nr. 70 C, pp. 169—171 :
Cuban Echinids ; Cenomanian to Coniacian.

Macstrichtian : Barrtttia monilifera Woodw., Parastroma sanchmi, cf. Pleskptys^matis hurcldmrdti Bocsc

Dordonian : Biradioliles cnbensis Dv., Titanosarmlitts gigantms (Whitf.), Torreiits sancbe^i (Dv )

Campanian : ? AntiUocaprina ? occidentalis (Whitf.): base of the Jamaican Rudist-bcd^'s.

Santonian : Biradiolites lumhricoJdes Dv., Dournonta cf. bourttoni (Dcs M.;, Boumonia cf. africana fDv ^
Bourtwnia hhpida (Dv.).nbsp;v

Turonian: Bourmma bispida (Dv.), Caprimda cubtnsts Dv. (= AntiUocaprina annuhta?) Plamttvcbiu
antillariini (Dv.).

This stratigraphy is untenable becausc of the coexistence of several combinations of fossils put into
different stratigraphical units by Douvill^; cf. C. T. Trechmann, 1924, Geol. Mac 61 nn '«8 quot;«Q •
M. G. Rim-en, 1936, Joum. Pal., 10, 2, pp. 134, 135.nbsp;^ 'nbsp;' '

O
§

O
O

Ä
w

►xJ

l-H

n
tt

G
►n

(T.) C de la Torr^ 1915, An. Ac. Habana, 52, pp. 824-827; (S.) M. SAnchez y Roig, 1926. Mem. Soc. Felipe Poey, 7. pp. 89-
rn'A « T^nbsp;m SAkch^, I.e., p. 102; (D.) H. Douvillé, 1926, B. S. g. F., (4) 26, pp. 127-138;

CD H.nbsp;\927. B.S.g.F.. (4) 27, pp. 49-56; (P.) R. H. Pau.,er, 1933, Rev. Agric Haban^M, nos. 15, 16, pp. 95-125

Undeterminable Radiolitinae and Ridist fragments: H 650, 668, 669, 670, 673, 7I6b, 716c, L 662
697, 698, 6Ô9; M 826, 827, 849, 873; V 461, 499, 500, 523.

Nerineidae : H 696, 697, 698 Ts 1007 (700 m S. of Aurora), Ts 1098 (=-- H670), Ts 1105, Najassa
(Douvillé 1927, p. 50, note).

Camerina dkk^rsoni (Palmer) : H 650, 689, 694, 697, 716b, Montejo, L662, 684, 697, 699, M 840,
873, Ciego de Avila.

11.nbsp;F. K. G. Muellerried, 1936, Bol. Soc. Geol. Mex., 9, 1, pp. 37^1 :
Rudists of Chiapas ; Ammonite-beadng beds are found between a
layer with Barrettia (Upper Turonian) and another with Pseudoharrettia
(Coniacian). The cretaceous complex extends farther upwards into the
Maestrichdan ff).

12.nbsp;J. Lambert, 1936, B. S. g. F., (5) 5, pp. 365—374, 376 ; Echinids
from Chiapas ; accepts Muellerried's stradgraphy. Most forms related
to „Senonianquot; forms. One, Linthia mullerriedi, related to a form, older
than Ripleyan.

13.nbsp;J. M. Muir, 1936, Geology of the Tampico Region, Mexico. Mexican
stradgraphy. The Cardenas-beds are contemporaneous with the Upper
Mendez (with Tampsia), and of Maestrichtian age, nec Campanian as
in Muellerried 1, c.; Sauvagesia degolyeri Stanton is put into the Lower
Santonian, nec Turonian as in Muellerried, 1. c.

14.nbsp;C. Burckhardt amp; F. K. G. Muellerried, 1936, Ed. geol. helv.,
29, 2. Ammonites of Chiapas. The determinadon of these Ammonites
forms the chief argument for Muellerried's stratigraphy.

15.nbsp;R. W. Barker, 1937, Ann. Mag. Nat. Hist., (10) 19, pp. 173—176 •
Foraminifera from Cardenas; Maestrichdan.

The authors are mainly divided into two camps. One for Maestrichtian
age the other (Echmid people and Muellerried for a much older age,
at least of the Barrettia-h^ds. On the base of the Cuban evidence I range
myself with the first group. This view has also been taken by my colleagues
on the ground of the encountered foraminifera.
The Cuban evidence runs as follows :
pological (cf p. 12). If the ^/;//W^-beanng limestones mendoned
are really mtercalated in the Tuff Series, an age older than Upper Coniacian
at the utmost, is out of the question, and a tectonical complication must
be assumed to exist in Chiapas, in which case Muellerried's chief argument
would become invalid.nbsp;^

Antillocaprina and Titamsarcolites. Comparable forms arc known from
the Campanian and Maestrichtian only (Rousselia and Trechmannella),

ft) Muellerri^ gives the following stratigraphical divisions:
Maestrichtian : Coralliochama.

Praeharrettia : again the only comparable forms, Pironaea, are Campanian
to Maestrichtian. As both the Antillocaprimnae and the Praeharrettiae have
been thought to be independent lines of development we cannot use them
for our purpose : although something may be said for the synchronism of
parallel development, it cannot be used as conclusive evidence.

Plagioptjchus was thought by Muellerried to point to a Cenomanian-
Turonian age. It will be argued on p. 154, note 6, that it is very doubtful,
whether the genus occurs in the Cenomanian, and its occurrence in the
Maestrichtian is beyond doubt f).

General aspect of the Rudists. To put forms like Barrettia into the
Upper Turonian, when the Hippuritinae were still in their cradle, is contrary
to all the fundaments of Palaeontology.

Loma Yucatan fauna. It will be seen on pp. 115, 118, that there is
good reason to assign a Campanian age to this fauna. The occurrence of
a variety of the Campanian Vaccinites inaequicostatus is the most obvious
argument for this.

Orbitoididae : such forms as Orhitoides and Lepidorbitoides point exclus-
ively to a Maestrichtian age. I found one only statement to the contrary
in the literature, and that was based upon a misquotation (Turonian for
Dordonian). The Loma Yucatan fauna, moreover, which is thought to be
Campanian is entirely devoid of Orbitoids. The coexistence of Orbitoididae
with Barrettia and its allies is definitely established : The original Pseudorhi-
toides trechmanni Douv. was pulled off from a Barrettia. M. G. Rutten
(1936, Journ. Pal., 10, 2, p. 134) mentions the occurrence of Pseudorbitoides
at the same locality as Barrettia monilifera. Thiadens (1936, K. Ak. Wet.
Amst., 39, 8, p. 1013) found Lepidorbitoides, Orbitoides and Vaughanina at the
same locality as Praebarrettia sparcilirata, and Pseudorbitoides and Camerina
dickersoni at the same locality as Parastroma sanche^i. I found Vaughanina
and Camerina dickersoni in the same rock as Parastroma guitarti in Camaguey
Province. I further observed in a slide through a Barrettia monilifera- bearing
limestone from Guatemala, not only an Orbitoid, which then was identified
as Pseudorbitoides israelskJ, but which may also belong to the genus Vaughanina-
described since, but also Camerina dickersoni. The occurrence of foraminifera

t) Plagioptychiu tihttiau Douv. 191G, and P. cf. aguilloiti in G. Astre, 1932, Hull. Soc. hist. nat. Tou-
louse, 04, 1, p. 88.

Lower Macstrichtian: Cardcnas-fauna, Orbitoids, Saavagtsia coloradmsis Steph., Tampsia bisbopi Stcph.,
Tampsia chocoyensis Stcph., Durania htmteca Adk., Dnrania aguHae Adk., CoraUiochama n. sp. of Mui-i.lkrriei)
(Muir, pp. 72, 74).

71nbsp;quot;nbsp;between Campanian and Upper Santonian: Sawagesia belli Steph. (Muir, pp.

Upper Santonian: Samagtsia morgani Adk., Durania manueltnsis Stcph. (Muir, p. 71).

The work of Muir is based upon a wealth of detailed information and inspires the greatest trust.

with „a complicated texturequot; is also mentioned from the Barrettia-h^^nn^
layers of Chiapas (10, p 162). The Cardenas beds contain a foraminiferal
fauna entirely comparable to that of Jamaica and Cuba (15) '

All this evidence points exclusively to a Maestrichtian age of the fauna
There is scarcely any doubt, but that the faunae of Cardenas, the Upper
Mendez, Chiapas, Guatemala, Jamaica, Cuba, and other AntHles, form one
and the same complex. I cannot but find them to be of Maestrichtian age
It may be noticed, that an entirely comparable fauna has been described

With this however, we have not refuted all the arguments of the
Echinid specialists and Muellerried. With regard to the first, we may
note, that some comparable forms have lately been described from the Upper

Muir) with Barrettta^n, p. 38), and other arguments, still have not been
overthrown. The evidence from Cuba, howeve^ is so ;xclusively in favour
of a Maestrichtian age, that I can but firmly held to the abovLxpressed

Orbitoids, and because of its total absence in the Loma Yucatan faum is
herewith considered to be an index fossil for the MaestricS '

The Eocene occurs in the North in two distinct fades : Cubitas (MilkliA
hmestones andnbsp;limestones (H 733, Loma C Hsif e ff

JUS possible of course that the difference is merely fad 1, but I have person-
ally he impression, that the typical Upper Eocene of H 733 oquot; rh« the

observed, but these observations are almost all near the SouthL boundaw
view is but meagre, and the suppo^rioVtmVet^T; ToT^Krquot;

The Cubitas Sierra has been mapped as „Cretaceousquot; by J. Whitney Lewis
(1932, Bull. Am. Assoc. Petrol. Geol., 16). This is evidently erroneous
not only because of the faunal assemblage, but also because of the tectonical
style.

The Eocene outcrops in the West and in the Sierra Maraguan are
similar in fades and fauna to the Northernmost Lepidocjdina-htoinng Eocene
although the presence of Lepidocjdinae could but rarely be demonstrated
(L 741). These limestones are mostly coarse, organic, with varying amounts
of detritic material. In the Maraguan Sierra we found finer-grained lime-
stones, which somedmes are opalized ; further mads, and nearly barren
fine-grained limestones with local reefs of corals (A 540). Another fine
grained limestone occurs at V 475 ; a fragment similar to this sample was
found in a nearby brecciaceous limestone of ordinary type (V473I) As in

^^u i 2' These fossils sometimes are disdnctly fragmentar}% in contrast
with the Eocene foraminifera found in the same rock (L 740a)
The following cretaceous fossils have been met with :
Rtidist fragments : L 740a, PL741, V473.
Camerina dickersoni D. Palmer : L 740.
Orbitoides: L740a.

Other detritic material: quartz, fdspar, biotite, diorite fragments
pegmatitic diorite fragments, porphyrite fragments of the Tuff Series

Faunal List. The Eocene limestones contain a rich fauna, on which
already several papers have been published by different authors. The species
described by them are pardy induded in the following list.

Camerina petri Rutten: H 733, 733a.
Camerina^)-. A540, L6G5, 740, 740a, V473, 475^, 486.
Cycloclypetts papulosa Hadlcy ¹) : near Nuevitas.
Opereulina ocalana Cushman *) : near Nuevitas.
OptrcuUna sp. «) : near Nuevitas.

Amphistegina cuhensis D. Palmer ») : H 733, Loma Calisto
Amphistegina lopt^trigoi D. Palmer: A540, LCC6. Rio Guanabanito
Ptllatispinlla : L 740a.

Dictyoconus'')-. L665, 666, M888, V473, 475^, 486, Loma Calisto«)
Lepidocyclina mtiiK^tri Vaughan : H 733.
LepidogcUna ocalana var. : Loma Calisto.
lepidocyclina cf. suhrauHni ') : Loma Calisto.

') The term Camerina must not be taken too strictly. So many forms of entirely different crouns show
a deceptive likeness to Camerinae in the slides, that one cannot be sure

') Described with several microforaminifera by W. H. Hadi.ev, 1934, Bull. Am. Pal., 20 nr 70A
„Near Nuevitasquot; stands for : In cut on railroad between Nuevitas and Pastelillo. about 15-2 kn N
of the Nuevitas railway station on Nuevitas Day.nbsp;'

») Only one specimen was found at locality H 733. Its radial section is an cx-irt mnv ^r n i-
mer's pi. 15. f. 2. (1934, Mem. Soc. Cub. Hist. Nat. 8 no 4)nbsp;^^ ' ^

Serpula cf. clytnenoides (Guppy): Loma Calisto quot;).
Lamellibrancbiata : H 733, L 665, Ts 1101 quot;).
Gastropoda^^): A531, 532, 534, 540, 542, L665, Ts 1101 quot;).
Bracbiopoda : H 703 «).

In addition to the foriminifera listed, we found some most curious
forms. One grows in a rounded cone,with a hollow core, like a raspberry.
Growth starts with one or two large embryonic chambers. A circle of
chambers of about equal size is plied below and against them, and new
chambers again in a circle against the last and so on. The latter' chambers
are more or less irregular. The whole is covered by a perforate layer.
It occurs at the localities A 540, L665, V473, 475i. Other aberrant
forms occur near the Rio Guanabanito in the Sierra de Maraguan. Amongst
them a Lepidocycline with double aequatorial layer, and compact lateral
layers.

Note on the extent of the Eocene: in the extreme South, East of M 888,
we have no proof, that the zone mapped as Eocene, really belongs to that
formation. The two samples M 850 and H695 are entirely devoid of fossils,
with the exception of Mtliolids and Lithothamnmm in M 850.

Age of the formation. The coexistence of Lepidocyclinae and Discocjclinae
at several localities marks an Upper Eocene age. The Cubitas Limestones
are thought to be a littie older.

a)nbsp;South of San Miguel de Nuevitas (V 447—453). The Pueblo itself may
yet be situated upon weathered Serpentine. Southward nothing is found
but greyish-black soil, 13,5 km long, and after that 10 km of dioritic sand.

b)nbsp;North of the Northernmost Eocene : a typical alluvial plain, used as a
landing-field for the Senado-planes.

c)nbsp;North of Central Senado : in a railway cut (H 737, 738), an enormous
conglomerate is exposed, which contains : Gabbro's, Serpentine, Camajan
Limestone, porphyrite-lava breccia, Camajan breccia of the Habana
Formation. Either a Tertiary or a Quaternary deposit.

Three tectonical phases could be demonstrated in this Province. They
coincide with tectonic phases found in Santa Clara and Pinar del Rio.

a)nbsp;The Pre Maestrichtian, Senonian, orogenesis. This folding is best
demonstrated by the Arroyo Hondo syncline, which disconformably
overlies Tuff Series, Serpentine and Diorite. It will be seen, that this
movement has also influenced the Aptjchi Limestones. Although this
orogenesis may partly have been contemporaneous with the intrusion
of Peridotite and Diorite, it must have continued for some time after-
wards, as is proved by the presence of Dioritic material in the Habana
Formation.

b)nbsp;The Pre Upper Eocene orogenesis. Its influence is demonstrated by
the structural difference between Cubitas and Camajan Sierra. A better
mstance still is the Western end of the Sierra Maraguan, where horizontal
Eocene overhes nearly vertical Habana Formation. The Habana Form-
ation both m the North and South has been strongly folded but the
movement must have been stronger in the North, as vertical Habana
beds have been wedged in between thé ^;)^r/;/-Limestones.

c)nbsp;Post Eocene movements. The Eocene has been folded by a distinct
but mostly weak orogenetic movement.nbsp;'

The presence of faults is indicated at several places. We find for instance
a dip of the transgressive Habana beds towards the older Tuff Scries in
the Ingenio Grande-Cantera Caballero zone at L 689, L 670 and L 671 The
same phenomenon was observed in the Eocene of the Eastern end of the
Maraguan Sierra, at its Northern boundary (A 545), and lastly all along
the Southern boundary of the Cubitas Mountains. The existence of a fault
here is so evident, that it has been indicated on the map. The age of this
fault and of that at A 545, is clearly Post Eocene. Whether the faults along
the Habana Formati^on are of the same age, or older, it is impossible to say
Ihe Camajan Sierra offers some curious problems. As we have here
several wedges of Habana Formation into the ^;,/j./.;-Limestones the
question arises why no wedges of Serpentine have 4en found. At first
si^ht one might be inchned to evoke a nappe-structure, to get out of tl
difficulty with ^^/gt;;-Limestones and Habana-breccia's as^one tectonic!
unit, and with the Serpentine as the other. There arc howeve scriou

of a nappe would not do us any good anyhow. Lastly, the chromite-chert
layer found at A 562, may present just such a scale of Serpentine. A much
more congenial hypothesis is, that the Pre Maestrichtian orogenesis had
already folded the ^^^'lt;r/6/-Limestones, just as it folded the Tuff Series in
the South, and that the subsequent denudation had already laid bare the
..^/)^^-/6/-Limestones, much as in their present configuration. So afterwards
the Maestrichtian was laid down directly upon the Neocomian Limestones
here, and upon the Serpentine elsewhere. If then we do not assign too
great an importance to the Post Maestrichtian folding, we may evade the
necessity of Serpentine-scales here. It may be noted, that Vermunt (pp. 33,
34) came to a similar conclusion with regard to the wedges of Habana Form-
ation in Pinar del Rio Province. Here too, a relative superficiality of the
overthrusting was assumed (Vermont, p. 34). Even so, a large number of
Serpentine wedges has been found in the Western Province, often accomp-
anying the wedges of Habana Formation. Vermont (p. 33) assumed, that
these correspond to Peridotitic intrusions into the San Andres Formation,
and that the overthrusting of the Habana Formation occurred by preference
along the soft and smooth surface of the Serpentine rock. So then we might
explain the absence of Serpentine wedges in the Camajan Sierra by the
absence of such Peridotitic intrusions here, which indeed is quite possible
seeing that the Peridotite had found an outlet all around the Camajan
complex. The supposed wedge at A 562 then would merely be part of the
surrounding Serpentine caught by the orogenetic movement; is it indeed
very near to the Camajan border. An alternative hypothesis is, that the
Serpentine wedges in Pinar del Rio Province correspond to a younger
intrusive phase, intruding at the time of the Post Maestrichtian folding.
The bulk of the Serpentine in the Western Province, however, must be
older in any case, as inclusions from the Serpentine have been found there
in Maestrichtian conglomerates.

Most of the older literature deals with the minerals found in this pro-
vmce. GoM has been mined in historical dmes (beginning of the sixteenth
century). Other metals mined are chromium, iron, copper and manganese.
Ihe occurrence of coal has already been mendoned in the Summary Salt
is made near Nuevitas. Asphalt occurs in the Sierra de Camajan. The Aptychi-
Limestones must be considered to be the source of this oil. Because of the
strongly folded and overthrusted tectonics of this Sierra, no exploitable
quantities of oil can be expected here. Near to the City of Camaguey we
were shown a curious occurrence of light oil. This oil is found in geodes
in achate in the Serpentine. The only feasible explanation of this curious
phenomenon seems to be, that the ^;gt;/j.^/-Limestones are present in the
depth, below the Serpentine; the oil shut off by the Serpendne seeps through
dong the , that ,re fiUed with chalcedone and achate, which imprisoL
the od in geodes. If this is true, the possibility exists, that oil ocLrs in

This part of the work is dedicated to the memory
of G. P. Deshayes, whose genius cleared the path
for the study of Rudists, and to the memory of
H. Douville, whose brilliant work has furthered
that study by such enormous strides.

L 702 : field observation number of Prof. Dr. L. M. R. Rutten.
A 540 : idem of Dr. A. A. Thiadens.
M 888 : idem of Dr. M. G. Rutten.
V 529: idem of Dr. L. W. J. Vermunt.
H 689 : idem of the author.
Ts835 : idem of Dr. Tschopp.
Museum numbers of the Mineralogisch Geologisch Instituut, Utrecht.
W70 : Pinar del Rio Province Collection.
N 10 : Northern Santa Clara Collection.
S 64 : Southern Santa Clara Collection.
Ca54 : Camaguey Province Collection.
Pa35. 1935: Palaeontological Collection.
For the technical symbols of the Rudists, I followed the custom.
An : anterior tooth.

Piv : posterior tooth (cf. Douvillé, H., 1936, B. S. g. F., (5) 5 pp
328—333, 335, 336).nbsp;gt; w , ff-

Au 2.nà Piv': anterior and posterior alveole.
3 : single tooth of the right valve.
lt;5' : its alveole.

The term Rudists is applied here to all descendants of Dicerasf).
The inverse Rudists were formerly classed into two subfamilies: the Gyro-
pleurinae and the Monopleurinae ff). This classification has been found
untenable. The writer is of the opinion, that the different forms belong
much closer together and that they do not fall into two sharply distinguished
groups. A groupmg into several phyla is much more natural. These phyla
can be roughly classed into three types of evolution. A full discussion of
the reasons for this view is given on pp. 94—105.

As the writer's interest was chiefly focussed upon the second and third
type of evolution, and as some restraint had to be put on somehow, the
study of the forms of this type has suffered in comparison. They could be
comparatively neglected, moreover, as important studies concerning their
Cuban representatives had already been published by SAnchez, Douville,
Palmer, Rutten, Thiadens and Vermunt i). In the following, a number
of more or less loose remarks are given, concerning some forms belonging
to this group.

Monopleurinae do not occur in the Habana Formation. The genus
Tepeyacia Palmer 1928, which occurs in the limestones, intercalated in the
Tufï Series in Southern Santa Clara, may belong to this subfamily (cf Thia-
dens, A.A., 1936, Proc. K. Ak. Wet. Amst., 39, 9, pp. 1133, 1134 ; text-
figs. 2, 5 (9, 10)). The Mexican genus Palus Palmer 1928 evidently belongs
to the Monopleurids. So possibly does the problematic form Baryconites
Palmer 1928.

Genus Biradiolites : The province of Camaguey is of special interest,
because of the occurrence there of many and varied small species of Biradio-
lites and Bournonia round about Ingenio Grande 2). Amongst them the

tt) Douvillé, Le., pp. 644-648; Paquicr, V., 1905, Mém. S. g. F., 13, 4 (Mdm. 29), pp. 50—53
1) SAnchez y Roig, M., 1926. Mem. Soc. Felipe Poey, 7; Douvillé, H.. 1926. B. S. c F (quot;4^ 26- Dnti
viLLÉ, H., 1927, B. s. g. F., (4) 27; Palmer, R. H., 1933, Revista de Agric., Habana, 14 nos 15 amp; 16-
Rutten, M. G., 1936, Joum. Pal., 10, 2; Tiiiadens, A. A., 1936, Proc. K. Ak. Wet. Amsterdam 39 8-
Vermunt, l. W. J., Journ. Pal. (in press).nbsp;' ' '

') As far as l could ascertain, Ingenio Grande is the same locality as San José de los Jibaros,

primitive looking Biradiolites lumhricoïdes Douvillé 1926 3). It must be stated
though, that more than one species occur at this locality, all very similar
externally, and all devoid of ligament and alveolar septum. B. lumhricoïdes
is the most common. A coarser ribbed, more Eoradiolifes-Yikamp; form with
thicker shell-wall, occurs at „Rio Blancoquot; at the foot of the Sierra Najassa
(Tschopp leg.) and also at Ingenio Grande (loc. H 698). A Biradiolites very
large for this type (length 110, diameter 42 x 35 mm) and externally exacdy
like Eoradiolites davidsoni Hill was found at Catadupa, Jamaica (Basel
Museum)

The Ingenio Grande fauna does not, as was thought by Douvillé s),
consist exclusively of these small forms. B. lumhricoïdes occurs around and
about such giant fossils as Titamsarcolites giganteus and Bournonia n. sect,
(loc. H 699). This association at the same time proves that they belong to
the fauna of the Barrettia-stmti.

Biradiolites cuhensis Douvillé 1926 was originally described from Arroyo
Hondo®). A similar Biradiolites but with only one interbande rib, was
collected by us at the Cantera Caballero, Camaguey Province, Cuba (loc.
H 670). It has one rib ventrally of E, and 5 dorsally of S. Dorsal cavity
large. Dendtion as in cuhensis. Structure dendculate. Not preserved well
enough to be named.

Other Biradiolites from America, also belonging to the acuticostatus-
group, or near to it, and with one interbande rib only, are'): B. aquitanicus
Toucas 8) from Charente, France, and from Cuba (Iocs. H624, just E. of
Fomento and L549, 12 km. NW. of Cabaiguan, both in Southern Santa
Clara, and from H 870, Verracos and M 938, 6 km NW. of Tranca, Pinar
del Rio Province), important for the correlation of the age of the Habana

{B. mooretownensis Trcchmann) SAnchez y Roig, M., Mem.'Soc. Felipe Pocy, 7, pp. 90. 91; PI.
1, f. 2. (containing a letter by Trechmann).nbsp;» m . .

a related or p^sibly identical form (cf. also Trechmann in lin. in SAnchez, I.e.. p. 91) is the B
Trechmann 1924 from Rio Grande, near Moorctown. Jamaica. Should the identity
firmed, then the name mooretonnensis would have priority over -Douvillé's name

bcloniT^'thtgLrJr^r^S:quot;quot;nbsp;ofnbsp;Trechmann 1924, which in its turn may

») Douvillé, H.. 1927. B. S. g. P.. (4) 21, p. 51.
Pl. i?f.Tnbsp;Whiteficld) sanchez y Roig. M.. Mem. Soc. Felipe Pocy. 7. pp. 89. 90;

Formation; and: B. subcancellatus Trechmann, fromjamaica. Two specimens
of the latter species are preserved in the Basel Museum, showing the curious
anterior groove 9). Other species with anterior grooves are: Boumonia
cancellata (Whitfield), and BiradioUtes adhaerens (Whitfield) lo). These grooves
have been compared by Trechmann (1924, Geol. Mag., 61, p. 403) to the
infolding of Tampsia. As this infolding occurs in the inhalent siphonal
band E, and not on the anterior side, they have nothing to do with it.

A fragment of BiradioUtes adhaerens, containing the ribbed inhalent
siphonal band E, was collected by Dr. Tschopp at loc. Ts. 450, 3,6 km
N. of Calabazar, Habana Province, Cuba. So by now the species has been
found in Jamaica, Cuba and Guatemala.

Genus Boumonia: A Boumonia, which may be reckoned to the species
''RadioUtes canceUatus'' of Whitfield, was found near Tio Pedro Camaguey
Province, Cuba (loc. H689). The anterior side of all three samples found
is imbedded in limestone, and in sections only traces of an anterior groove
could be found, but then, in the Jamaican samples, the grooves appear to be
faint. Douvillé 1927 (B. S. g. F., (4) 27, p. 50) says, that this species has
one interbande rib or fold. In Whitfield's or Trechmann's descriptions I
could find nothing of this, and Whitfield's PI. 13, figs. 3, 5 clearly show,
that there is no rib, but only a groove, so that the species must be reckoned
to the genus Boumonia n). The cuban samples are a little larger (up to 80 mm
length, diameter 60 mm). The three forms hispida Douvillé, tbiadensis Ver-
munt and cancellata are very similar. In tbiadensis and cancellata, the body-
cavity curves outward at the siphonal bands, in hispida not. B. cancellata is
the largest of the three. The „BiradioUtes aff. cancellatusquot; of SAnchez Roig
from Arroyo Hondo, belongs to the BiradioUtes cubensis Douvillé. The
Cuban Boumonia cancellata are associated with Miliolids, Camerina dickersoni

D. Palmer 12)^ Orbitoides, Titanosarcolites giganteus and Bournonia (n sect W
Genus Bournonia, new section (textf.; PI. 8, f. 10): Our collections contain
a new type of Bournonia, characterized by the nature of the siphonal region
£is a broad, flat-bottomed down-fold of the funnel-plates. At the posterior
side of the funnel-plates slope suddenly and dizzily upwards. The highest
point IS reached at the exhalent siphonal band, where they form a flat
narrow, shghtly depressed top, to slope downward, but not as deeply again'
on the other side of the J. On the surface the E is marked as a broad ledge'
crossed by numerous distinct growth-stages. I is a groove, and J' forms'
the top of a rounded rib. The lines, which in a horizontal section delimit
the siphonal area J, converge outward. That part of the shell, which corres-

Horkontal section through
Boumonia nov. sect. sp. 4
(Ca 252), collected at locality
H 689, near Tio Pedro. Note
the comb-likc aspect of the
scptatcd myophore, and the
scptac of the right valve
fitting between those of the
myophore. Natural size.

(about 20° in thenbsp;30°T, J n ^quot;Cquot;quot;quot;'/'quot;''quot;'quot;quot;quot;'

^t were into sLies of points ortr^fet^afr l^ontl
ft .llw's'lfanbsp;Snbsp;«'C. a™,..,0.2, pp. ,91 .92- gt;., 2

sections (denticulate structure i^). Left valve flat and plane except in the
siphonal region, where it follows the foldings described above. Its structure
lamellar, subnacreous. Myophores large, septated with great regularity,
comb-like in sections. The inner shell layer of the right valve, here forms
corresponding septae, fitting in between those of the left valve (cf textf )
In this way the surface for muscle-attachment is enormously enlarged.
This feature, by the way, is developed in many different Radiolitids. Habitus
of a Biradiolites (cf. B. praeingens Toucas).

Some species attain enormous size, up to 620 mm diameter, and still
larger. These giants were found near Ingenio Grande, accompanied by the
small Biradiolites lumhricoides. The different species of this section are very
uniform externally, and can scarcely be distinguished, but by their average
size, and by their structure is). The following species belong to this section :

type locahty ; loc. H 241, H 245, near Abra de Castellon, all in Southern
Santa Clara, Cuba).

3.nbsp;Bournonia n. s. Thiadens 1936 (loc. H 601, near Fomento, Southern
Santa Clara, Cuba).

4.nbsp;Bournonia sp. (textf; PI. 8, f. 10) (loc. H 689, near Tio Pedro; Ts. 1091
near H 689; H 694, 3,5 km N. of Esperanza; all in Camaguey, Cuba)
Prisma-cell walls continuous, not denticulated; structure almost irregularly
reticulated, radially arranged in places only. Associated with Orbitoides,
Camerina dickersoni, Bournonia cancellata, and Titanosarcolites giganteus at
loc. H 689, with Camerina dickersoni at H 694.

5.nbsp;Bournonia sp. (loc. H 697, near Ingenio Grande, Camaguey, Cuba);
giant species (see above), structure vermiculate, rather coarse, branchings
of vessel-impressions comparatively wide in places.

Fragments of fossils also belonging to this section were found at Iocs.
M 840 (see map) and L 684, Sierra Najassa, both in Camaguey, Cuba. Note
further the occurrence oï „Radiolites nicholasi'' on St. Domingo, St. Croix
and in Peru^®).nbsp;'

») cf. Douvillé, H., 1927. D. S. g. F., (4) 27, pp. 55. 56. Mac Gillavry's remark (Proc. K. Ak. Wct.
Amst., 35, à, p. 387) about this structure was based upon a misconception, and is rctracted herewith For
a discussion of the structure see also: Rutten, M. G., 1936, Joum. Pal., 10. 2. p. 138. The denticulated
structure is of so common occurrence in the genera Biradiolites and Bourtionia, that we may safely reject
Douvillé s genus Parabournonia, based upon this feature only.

gt;«) cf. Thiadens, A., 1936, Proc. K. Ak. Wet. Amst., 39, 8, Pl., ff. 6,8 and 7 9.
quot;) Bournonia (n. sect.) nicholasi (Whitfield).nbsp;'nbsp;'

(1921 {Radiolites sp. similar to nicholasi) Stanton, T. W. in Cooke, W., Geol. Surv. Dominican Reo
Mem. 1. p. 55 (Santo Domingo).

(1923 {Radiolites n.) Stanton, T. W. in Vaugiian, T. W.. J. Wash. Ac. Sc., 13, no. 14 n 305 fSt
Croix).nbsp;' ' ■nbsp;■

1926 {Upeirousia n.) SAnchez y Roig. M.. Mem. Soc. Felipe Poey. 7. pp. 85. 91—93, 102 (p. 102-
Douvillé in litt.: =Bourtwnia nov. sp., not to be found, however, in Douvillé 1926 C. R. S. g. F.. to which
this passage refers, but in SAnchez's own paper on p. 93) (Cuba).
(1932 {Durania «.) Kühn, O., Foss. Cat., 54, p. 108.

1934 {Sphaerulites {Lapeirousia) cf. /;.) Olsson, A. A.. Bull. Am. Pal. 20. no. 69, pp. 47, 49, 50; PI. 1
f. 2; 8. f. 4 (Peru).nbsp;gt; . i • gt;

The outer shell-layer in this section is not resistant, and samples are
found with the shell worn away almost down to the body-cavity. Such a
sample (Ca. 249) found at loc. H 689 looks like a cylindrical Radiolites
externally. It is quite possible, that Radiolites galojrei Palmer presents just
such a case. It was found in the Sierra de Najassa, the western continuation
of the cretaceous zone of loc. H 689.

The origin of this section is obscure. The siphonal development of
Praeradiolites ponsianus var. aegyptiacus Douvillé 1910 presents similar points,
but this may be regarded as a convergence. The aegypdan form has a dis-
dnct ligament. Bournonia haydeni Douvillé 1916 and Bournonia mutahilis
(Stoliczka) have structural affinities, but the nature of the siphonal region,
at least that of haydeni is different. Biradiolites macgillavryi Vermunt (193?'
Journ. Pal., in press) from loc. H 802, 1,5 km WSW. of San Diego de los
Banos, Pinar del Rio Province, Cuba, gives the impression of being inter-
mediate between Biradiolites and this secdon, and it is indeed not impossible
that the section may have originated from that genus.nbsp;'

Genus Tampsia : Of great importance for the correlation of the Habana-
formation IS the occurrence on Cuba of the Mexican genus Tambsia repre-
sented at two distinct localities by a new species i')nbsp;' r

Genus Durania : Of great paleontological interest is the occurrence at
Loma Yucatan, Camaguey Province, Cuba, of Durania curasavica (Martin)
originally described from Curaçao is). At the Cuban locality it occur
with its characteristic flat shape, in the company of a cylindrical species •
Dur. lope^-trigoi (Palmer)-). There even is i'n oL collections a ^
one ƒ curasavtca and two D. hpe^-trigoi growing together. As a result
the flat shape of D. curasavica is a true specific featurt and not to be ex^
plained from outer influences. It has not been generally understood ^o) that k
attains great size. The greatness of its size is illustrated by the large into
bande fragments figured in the paper citedi«) (e.g. PI. 2, fig. 4) Onlv the
larger specimina could not be extracted from the rock at Curaçao Therefore
a small, but intact sample was chosen as type specimen. Nevertheless s^e-
amens of about 300 mm diameter must be faidy common the Fr^m
the Loma Yucatan, we brought home with us two large spcc minaTf
respectively 290 by 300 (Ca. 197) and 250 by 300 mm^ Ca^T^ The
body cavity of the first has a maximum diameter of 160 mm Tl e nvo
species curasavica and lope^-trigoi are sharply distinguished by^helr stmc

those of curasavica about I mm or more. Palmer's species was described
from a badly weathered specimen. We have a number of specimens
(Ca. 220—236, loc. V529, Ca. 224 donated by Mr. Lopez Trigo). The
species may be described as follows:

In youth widely spreading in a low cone, becoming afterwards cylin-
drical to subcylindrical, sometimes rather suddenly. Smallest diameter
through I. Test thick (in Ca. 223, diameter 115 : 22 (through E) to 45 mm
(at the dorsal side) ; body-cavity 50 (through E) by 38 mm). Surface covered
with regular ribs, at about 2 to 3 mm from the top of one rib to the next.
The ribs sometimes duplicated. Growth stages numerous, often at about
4 mm inter se, but not very prominent. S developed as the more or less
flat, slightly depressed top of an often quite sharp upfolding of the funnel
plates. It is set off at the edges by a small, but sharp downward flexure
of the funnel-plates, hence the word depressed. In some cases the funnel-
plates form a fold in the S itself as well, mostly an upward fold, prolonging
the slope before and behind it, but sometimes a downward fold. The breadth
of S varies from 7 (Ca. 232, diameter 50 mm at the corresponding height)
to 16 mm (Ca. 221 and 222, diameter 110 both). £'also is a slight depression
of the funnel-plates, set off at the edges by a similar downward flexure of
the plates. It sometimes forms the top of a comparatively unimportant
upfolding, but generally, the plates remain horizontal right up to its edges.
I forms a slack downfold of varying amplitude. B is flush with the test,
a depression or a distinct indentation. S similar to B, but often a little
more depressed. / is a ridge, which has a rather sharp bend at the point
where the growth changes over from the conical towards the cylindrical.
Both siphonal bands were probably covered with a number of small ribs.
Traccs of these were found in one case only (Ca. 234, inhalent siphonal
band, three ribs, at 0,7 mm from top to top, giving a total of 10 ribs for
this band). The I is covered with ribs of normal size. Again some of them
arc bifid. The thickness of the funnel-plates varies from 0,3 up to 1 mm,
averaging 0,6 mm. Undulated near the outer rim, a downfold corresponding
to a rib. Slightly curved in profile, convex towards the commissure, making
an angle of 70° (near the body cavity) to 80° (near the surface) with the
shell's axis -i). Prisma-cclls rather small, their diameter averaging 0,5 mm.

D. palmeri Vermunt-) from Central Bahia Honda, Pinar del Rio
Province, Cuba (loc. V843a), may be identical with this spccies. The
diflcrence in conservation makes it hard to judge.

D, curasmca is mainly characterized by the following points : widely
spreading in a low conc; siphonal bands with numerous smaller ribs. In
the Cuban samples I counted up to 28 for the S, and more than 18 for the E,
S flush with the test or a shallow depression ; E at the bottom of a deep,
mostly asymmetric sinus, sometimes almost occluded (in the large samples).
Funnel-plates horizontal, plane, tangentially as well as radially (except near

*') The anRlc between funncl-platc« on both sides of the body cavity u-as measured, and divided in half

the body-cavity and near the surface), with two flat-bottomed, steep-edged
folds corresponding to the siphonal bands, their edges converging outwards.
Thickness of the funnel-plates about 0,4 mm, but occasionally much greater,
so that the samples with thick funnel-plates from Curasao, remarked upon
on pp. 385 and 387 of the type description, may quite well belong to the
same species. Angle of the funnel-plates with the shell's axis 85—100° 21).
Prisma-cells : 0,9—2,4 mm, averaging 1 mm. The upper valve fragment,
figured on PI. 2, f. 5 of the paper cited 1®), has been cut through radially.
Its structure is compact, laminar.

The Durania sp. B of Vermunt (same locality as D. palmeri) may
possibly belong to this species, and so may the ill-preserved fragments of a
Durania sp. from loc. H260 Gavilan, Southern Santa Clara, Cuba, briefly
described by Thiadens ^3).

The Durania sp. A of Vermunt is of a different type altogether, with
sharply folded funnel-plates.

Genus Chiapasella \ This curious genus has not been encountered in
the Province of Camaguey. The note by Boissevain, H. amp; Mac Gillavry
H. J. (Proc. K. Ak. Wet. Amsterdam, 35, 10, 1308—1312) dealing with
this genus, contains some errors. The cortex (c) on fig. 5 does not belong
to the animal at all, but is an attached organism, as was observed by me
afterwards in a slide. There is no cortex at all in this sample, and its structure
remains prismatic almost up to the surface. This explains, why we did not
find any cortex in the infolding. In another specimen (loc. H 774 5 km
NNW. of San Juan y Martinez, Pinar del Rio Province, Cuba) a cortex
(compact outer part of the outer shell layer) was found, which indeed
follows the infolding. Apparently some specimens have a cortical outer
part of the outer shell layer and some not. This explains the difference
between Muellerried's observations and ours. On fig. 6, the J' and E
have been put in the wrong place, as was pointed out by Rutten M G
(1936, Journ. Pal 10, 2, p. 140) The specimen figured has 12 infoldings'
It is true, but only 9 larger, and about 3 smaller ones. So the material is
not intermediate between the species radiolitijonms and pauciplicata but
conforms exactly to Muellerried's description of the latter species So
our argument for suppressing this species is invalid, and the Cuban material

of the shell laU (193i An. Ins't. BiTlltrquot;
to n.e erroneous. The outermost laminar layer of the left va ve 1st be
paralleled to the prismatic layer of the right one. They form thToute
shell layer. In this way it becomes clear that the superposit o^of the she!
laj^one valve upon the other is quite normal. This at tL same time

shows, that the fibrous layer of the Caprininae really conforms to the prism-
atic layer of the Radiolitinae. The canal-bearing layer of the left valve, belongs
to the inner shell layer.

Ligament-bearing Radiolitids: A ligament-bearing Radiolitid was
found at Ingenio Grande (loc. H 697). It is ill-preserved and undeterminable,
but seems not to belong to Radiolites macropUcatus Whitfield . K good
description of that species is found in Thiadens (1936, Proc. K. Ak. Wet.
Amst., 39, 8, pp. 1013, 1014; textf. 3 (4, 5); PI., ff. 4, 5). The material
described by Whitfield is heterogeneous. Only the large specimens (PI. 12,
f. 2 ; 13, f. 8) conform to the type described by Thiadens. The small sample
of PI. 14, ff. 1,2, belongs to the genus Biradiolites. The samples of PI. 12,
f 3 either to Bournonia or to Biradiolites.

Ligament-bearing Radiolitids are more common in the northern part
of Santa Clara (near Sagua la Grande). M. G. Rutten mentioned the
occurrence of Saiwagesia from this region (1936, Journ. Pal, 10, 2, p. 135),
but there are also found forms with radially stretched canals, so that still
other genera are involved.

The following subfamilies (or tribes) : IchthjosarcoUtinae, Trechmannel-
Imae, Kousseliinae, Antillocaprininae, Lithocalamus, Immanitas and Hippuritinae
have always puzzled the scientists that occupied themselves with Rudists
and, as a consequence, have been spread all over the Rudist system. They
are put together here for the first time in an attempt to solve this problem.
They are treated m different subfamilies, because they are not, it is thought
direct y related to one another, but aUied in so far, that they followed tiie
same lines of change. So they form a group in the very sense of the word
They are characterized by the following features : the inner sheU-layer
ot at east one valve, is traversed by numberless canals that are rounded
or polygonal in section. In the Hippuritinae this holds only for the left
valve of Torreites, but this well-known subfamily for reasons to be disclosed
later must be mcluded into this group. In all but Torreites and the Ichthyo-
sarcohttnae these canals, at least those near the visceral chamber are crossed
at interva s by transverse tabulae f). The single tooth 3 of the right valve
is reduced and its alveole in the left valve, if present, is not extended into
an accessory cavity. The outer shell-layer seems to be entirely reduced in
all but Rousseha, Trechmannella and the Hippuritinae. In Rousselia it is at
least greatly reduced. Only problematical traces of it were found in a voun^
Antillocaprina (c£ PL 1, f. 1; 9, f. 4). The dentition varies, depending on the
stage of evolution reached. In such forms as have only one shell-layer
the position of the teeth leaves no doubt, but that it is really the inne^
shell-layer. Only in the case of Ichthjosarcolites there remains some doubt.

The genus is listed in both catalogues (Kuhn and Kutassy Foss Cat
54 amp; 68). In both the bibliography is insufficientiy treated.' Important
works like that of Deshayes 1825, and Douvillé 1888 have been omit-
ted, whereas others that contain nothing much of interest are listed So I

diaphragms as cross the direction of growth, to avoid confusion
pit^clldiSr'nbsp;^ 'nbsp;of a Caprinid left valve, and%r the'eardbdseprm'of

Others containing short diagnoses or a discussion on the systematical
position (older literature) have been left out, except if a synonym is in-
volved (de Haan), or when a figure is given (Pictet, Chenu), even if
this is but a copy of an older figure. This for convenience's sake.

(Cucroides) Guettard, J. E. — Nouv. coll. de mém. sur diff. parties
d. sc. et arts, 1, Paris, 14me mém., pp. 552, 553; PI. 28, f 2.
(Ichthyosarcolites triangularis) Desmarest, M. A. G. — Bull. d. sc.
phys. méd. et d'agric. d'Orléans, 5, p. 324.nbsp;i)

(Ichthyosarcolites triangularis) Desmarest, M. A. G. — Journ. de
phys. chim. hist, nat., 85, pp. 45, 50, 51 ; PI. 2, ff. 9, 10.
Defrance, M. de — Diet. sc. nat., 19, „Glossopètresquot;, pp. 72, 73. 2)
Defrance, M. de — Diet. sc. nat., 22, „Ichthyosarcolitequot;, pp. 549,
550.nbsp;3)

(Ichthjosarcolithes triangularis) Blainville, H. M. Ducrotay de —
Diet. sc. nat., 32, „Mollusquequot;, p. 191 ; PI. 12, £ 1 ; PI. 20, f 2
(the figures of one plate identical with those of the other). ^^
(Ichthyosarcolites triangularis amp; obliquus n. sp.) Deshayes, G. P. —
Diet, class, d'hist. nat., 8, „Ichthyosarcolitequot;, pp. 499—501.
(Rhahdites = Tiranites (Baculites) -}- Ichthyosarcolites) Haan, W. de —
Monogr. Ammonit. et Goniatit. sp., Leiden, pp. 40, 41, 52, 53,
57, 160.

(Ichthyosarcolites-, J. angularis) Orbigny, A. Dessalines d' — Ann.
sc. nat., 7, pp. 167, 168.

Rang, A. Sander — Manuel de I'Hist. nat. d. mollusques, Paris,
pp. 96, 300.nbsp;5)

Roulland, F. — Actes Soc. Linn, de Bordeaux, No. 21 (4, 3e livr.),
pp. 164—166.nbsp;6)

'1786

*1812

1817

^1821
1821

1824

^1825

1825

1826

1829

1830
1830

*1829,

1849 (Caprinella t. amp; Douhlieri n. sp.) Orbigny, A. d' — Paléontologie
française terr. crét., 4, Atlas, Pl. 541, ff. 1, 2 (doublieri)- PL 542
11. I—[triangularis).
^1850 id. id., text, pp. 189—191.nbsp;J

1851, 1852 (Ichthjosarcolithus) Bronn, H. G. — Lethaea geoenostica 3 d
edition, 2 pt. 5, pp. 251-253; PL 31, f 5 (copied from de Blain-
ville) ; PL 31, f. 4 ab (copied from d'orbigny 1849, PL 541 ff 1 2) n)
1855 (Caprinella united with Caprinula) Woodward, S. P — Quart

Journ. Geol. Soc., 11, pp. 52, 53; textff. 25—27 (fig. 25 after d'OR-
BiGNY 1849, PL 542, ff. 1, 2).nbsp;^ ^nbsp;L

Atlas, PL 89, f. 15 (copied from d'Orbigny 184 9 PI 542' £ 1)
1862 rQCHENU,J.C. —Manuel de Conch, et dePaL conch 2'p 239-
textf. 1216 (copied from d'Orbigny 1849, PL 542 f 1)
* 1865 (C. bicarimta n. sp.) Gemmellaro, C. - Atti Accad. Gioenia
_Catama, (2) 20, p. 26; PL 4, ff. 5, 6.nbsp;u)

name douMkri occurs for the first time in the pLes of Sal S te fl icutsIsQ-lS Sq'? V^
Jahrbuch etc. 1850, p. 52 and C. D. Sherborn, Geol. Mag. 1899 p IS As S^k^
of the text only. I give here the complete data for the fourS vSe'^'of thequot; Terr S 1X17quot;

For corroborative evidence see: Tallavignes (B. S. g. F., (2) 6 o 285 séance ^ TT 1R4Qgt;, tu j •
livrakonquot; at that date, contained plates or a plate of^/Z^^iî^^ hlïirg the
thenbsp;plates are: 526-535, the plate referred to being either d1 527 or^-^4^ rf oi ^^^^^ ^

quot;) On p. 252: „De Roquan 1831quot; is an error for Roulland 1830 Deframpr i»nbsp;-.a u

author of the figure copied on PI. 31, fig. 5 (cf. note 4)nbsp;-Uefrance is wrongly citcd as the

_ quot;) The spiral valve (fig. 25) is taken for the left valve. In fig. 26 the tabulae are drawn to curve back
I^ThTtw?' 'nbsp;is.contrary to the figures of Desmarest and ^TB^Z^ t

quot;) In the first edition, vol 3, 1845, p. 400 „Desmarets (Bull. Soc. Linn, de Bordeaux t I)quot;
IS a confusion with Desmoulins.nbsp;ooraeaux, t. i)

1887 (L, united with Caprinula) Fischer, P. — Manuel de Conch, et de
Pal. conch., pp. 1057, 1058; textlF. 804A—C (idendcal with Wood-
ward's figures).nbsp;i®)

1887nbsp;(I., two species) Douvillé, H. — Bull. Soc. géol. Fr., (3) 15, pp.
759, 791—793; textfF. 15—17.

1888nbsp;Douvillé, H. — Bull. Soc. géol. Fr., (3) 16, pp. 706, 728, 729.
^1890, 1891 Thomas, P. amp; Peron, A. — Descr. moll. foss. terr. crét. région

^(1910 (I. sp.) Paquier, V. amp; Mengaud, L. — Bull. Soc. géol. Fr., (4)
10, p. 528.

'^(1916 (I. caput-aequi? amp;c hicarinatus) Parona, C. F. — Rendiconti R. Acc.

Lincei, (5) 25, p. 272.
quot;1921 (I. triangularis, hicarinatus Se tricarinatus n. sp.) Parona, C. F. — Mem.
descr. carta geol. It., 8, pt. 3, pp. 9—13; textff. 7—11 ; Pl. 1, ff. lab
(triangularis)-. Pl. 2, £ 1 (hicarinatus) amp; 2 (tricarinatus).
1922 Harris, G. D. amp; Hodson, F. — Pal. am., 1, No. 3, p. 128 i»)
'M 926 Parona, C. F. — Mem. 1st. geol. R. Univ. Padova, 7, p. 40.
1930 (C. tr.) Repelin, J. — Descr. géol. succ. Dép. Bouches-du-Rhône,
Encycl. départementale, 1, Pl. 7, f. 5.

Distribution of genus: France (Charente-inf., Charente, Dordogne,
Maine-et-Loire, Deux-Sèvres, Vienne, Bouches-du-Rhône)^; Italy (Gargano)
Sicily^; Spain (Altamira de Sandllane)'; Bulgary (Lom valley)^'^ 20).
Istda (Pisino)quot;'; Tripolitania''-Tunis southern^^-«Se central'quot;.

Vertical range: Urgonian (Upper Barrêmian-Aptian, cf Paquier
1905, p. 99); Upper Albian (cf p. 50: „Portugalquot;); Cenomanian; ??Maes-
trichdan (cf. p. 53, ?/. sp.)

The following is a list of other localities mentioned in the literature,
but uncertain through lack of description. N.B. Altamira de Santillane has
been included above on the authority of Paquier. The American forms are
dealt with separately.

'•) In Douvii.lI^'s abstract of this paper in the Rev. crit. de Palöoz., 7, p. 153, 1903 : „au-dessusquot; is
an error for au-dessous.

quot;) 1905 is the date of publication and not 1903 as in Kühn, Cat., pp. 115, 116.
quot;) 1914 is the date of publication according to Parona 1921.
quot;) Here the genus is wrongly stated to have canals in the lower valve only.
'quot;) The localities RugCuk and Besarbov are also situated on the river Lom.

etc. Bologna, (2) 3, p. 444 (Venetian Alps),
nec 1892 (L sp.) Futterer, K. - Pal. Abh. Dames amp; Kayser fn f^
2, 1, p. 105 (Calloniche).nbsp;^ ' ^

The first reference without description. The second with sufficient
description to see, that it cannot refer to an Ichthjosarcolites.

1855 (Caprinella triangularis) Spada Lavini, Al. amp; Orsini — Bull Soc
géol. Fr., (2) 12, p. 1208 (Appenine Mts.).nbsp;' '

1897 (L triangularis) De Angelis d'Ossat, — Boll. Soc geol It 16
pp. 284, 285 (Monte Affilano).nbsp;quot; ^ ' '

1908 (I.) Parona, C. F. — Boll. Soc. geol. It. 27 d 302 fid ^
''''nbsp;~nbsp;g-l'lt. pt 1, p. 40

mist.?'^^ther irregular
prisma-cells The second without description. The remaining four refer

*I859 (Hippurites traguriensis) Lanza, F. - Viaggio in Inghilterra etc
Ca? p 7?nbsp;' ' 2 — ' (Ichthjosarcolithïs?) Kûhn,0:;

sous-Pyrénéenne des Basses Pyrénéesquot; •
1891 (I.) Seunes, — Bull. Soc. géol. Fr., (3) 19, p. XXII.
Without description.

1897 (I triangularis) Choffat, P. — Bull. Soc. géol. Fr. (3) 2 n 471
Without description.nbsp;' ^ '

1905 (U.) Paquier, V. — Mém. Soc. géol. Fr., 13, 4 (Mém 29) n 95
(^/.;^^Paquier, V. amp; Mengaud, L. — Bull. Soc. géol. Fr.f(4) 10^

„sections d'un Rudiste qui paraît être, selon toute probabilité un / quot;
(Djebel Debar, Blayac leg.).

SW. Teile d. persischen Golfes, p. 18.
(1929 (cf. c. d.) Kuhn, O. — Ann. Nath. Mus. Wien, 43, p. 17.
(1932 (cf. c. d.) Kuhn, O. — Ree. geol. Surv. India, 66, p. 173.

Without description. Khamir on the Persian coast, N. of the isle of
Kishm (Quishm).

There may be many another reference of this kind. The above have
been mentioned to stimulate more collecting and investigation in the lo-
calides named f).

The following old-world species belong or may belong to this genus :
I. hicarinatus (Gemmellaro) Douvillé.
1865 (Caprinella hicarinata) Gemmellaro, C. — Atti Acc. Gioenia Catania

(2) 20, p. 26 ; PI. 4, ff. 5, 6.
1888 Douvillé, H. — Bull. Soc. géol. Fr., (3) 16, p. 706 („La Caprinella
hicarinata est toutefois, d'après toutes les probabilités, un Ichthjo-
sarcolithusquot;).

1898 Douvillé, H. — Bull. Soc. géol. Fr., (3) 26, p. 149 („ . . paraît
se rapporter à un Ichthjosarcolitbusquot;).
^(1914 (Ichthyosarcolites hicarinatus) Parona, C. F. — Atti R. Acc. Se.

Torino, 50, pp. 20, 21, 22.
^(1916 Parona, C. F. — Rendicond R. Acc. Lincei, (5) 25, p. 272.
^1921 Parona, C. F. — Mem. descr. carta geol. It., 8, pt. 3, pp. 12 13-
textff. 7, 10 ; Pl. 2, f 1.
Upper Cenomanian (Parona 1921, p. 5).
Sicily'-quot;' (type locality); Monte Gargano^'Tripolitania^-
N.B. Gemmellaro's type has been re-examined by Parona.

I. douhlieri (d'Orbigny) Bronn ^i).
1849 (Caprinella Douhlieri) d'Orbigny, A. — Pal. fr., terr. crét., 4 Adas
PI. 541, ff. 1, 2.

'1850 d'Orbigny, A. — Pal. fr., terr. crét., 4, Text, pp. 191, 192.
nec 1850 (Caprinula douhlieri) Sharpe, D. — Quart. Journ. Geol. Soc.,
London, 6, p. 180; PI. 17, ff. 3, 4 (= Caprinula olisiponensis
(Choffat) 1885.

1851, 1852 (Icbthyosarcolitbus) Bronn — Lethaea geogn., 3d. ed., p. 252 2i)
^1905 (Ichthyosarcolithes D.) Paquier, V. — Mém. Soc. géol. Fr., Pal.,
13, fàsc. 4 (Mém. 29), p. 95.
?*1926 (c. cf. duhlieri) Douglas in Richardson (cf this p.: „Persiaquot;).
Cenomanian^.

France (Bouches-du-Rhône: Martigues)'; PPPersia.
_RB. d'Orbigny's type-specimen was seen by Paquier.

t) For instance Ichthyosarcolites ? sp. from Ostuni, Brindisi, Italy in Zuffardi-Comerci R _

quot;) The species is not named there, but unequivocally referred to. Afterwards the species was named
under the generic heading of /. by Gabd, W. M., 1861, Proc. Am. Philos. Soc., 8, No. 65, pp. 239, 242.

1825 (Ichthyosarcolites obliqua) Deshayes, G. P. — Diet, class d'Hist
nat., 8, p. 501.nbsp;' 'nbsp;quot;

No explicit statement on the locality is given by Deshayes, but appar-
ently It hails from the neighbourhood of La Rochelle. Roulland saw the
species m the collection of the „Cabinet d'hist. nat. d'Angoulèmequot; Again
no locality is mentioned. The age may be taken as Cenomanian. A forgotten
species. As Deshayes, later (Enc. Méth. d. vers, 2, p. 312), regarded the
genus synonymous partly with Caprina and possibly partly with Hipturites
he did insist no more upon this species. It must be noted, that Douvillé
l»«7, again mentions the occurrence of two species differing in size.

Type locality: In the type description of the species triangularis no
locality is mentioned. Guettard's' material came from the neighbourhood
of Rochefort, Favames leg.quot;, Defrance^ names : He d'Aix and the neigh-
bourhood of Rochefort; Deshayes^ neighbourhood of La Rochelle The
other french locahties, wkh the exception of Vienne, have been listed by
dOrbignyI Mentioned from Vienne by Gilles de la Tourette, 1844^

g. t., (2) 2, pp. 52, 53 (see also A. de Grossouvre, 1889 B. S g F '
(3) 17, p. 522.nbsp;' •amp;••■gt;

L tricarinatus Parona 1921.
'gt;{\^\^(Lcaput-aequi^) Parona, C. F. — Rendiconti R. Acc Lincei

1921 (L tricarinatus) Parona, C. F. — Mem. descr. carta geol It 8
pt. 3, p. 13; text ff. 8, 11 ; Pl. 2, f. 2.nbsp;^ quot; ' '

Monte Gargano, Tripolitania. (Monte Gargano may be regarded
as type locality.nbsp;^ h ^^

1887 Douvillé, H. - Bull. Soc. géol. Fr., (3) 15, p. 793 („Les échantillons

(1901 Paquier, V. — Bull. Soc. géol. Fr., (4) 1, p. 286.
(1903 Douvillé, H. — Rev. crit. Paléozool., 7, p. 153
1905 (Ichthjosarcolithes sp. nov. indét.) Paquier, V. — Mém. Soc. géol. Fr.,
Pal., 13, fasc. 4, (Mém. 29), pp. 94, 95, (98); Pl. 9, figs. 7—9.

Urgonian (Upper Barrêmian-Aptian, cf. Paquier 1905, p. 99).
Bulgaria (Valley of the River Lom : near the „Moulin Guérowquot;,
Ruscuk and Besarbow).

Species incertae sedis:
?I. marginatus Pocta 1886.
1886 (I.m.) PoÖTA, F. — Sitzber. k. böhm. Ges. Wiss., p. 207.
1889 (?I.m.) PocTA, F. — Rozpr. k. ceske spol. nauk. 7, 3, pp. 68, 87, 92;
PI. 6, ff. 6, 7.

Vide p. 50 „Appenine Mts.quot;: 1897 De Angelis d'Ossat; 1908
Parona ; 1909 Parona ; 1911 Parona. (cf also 1855 Spada Lavini amp;
Orsini).

N.B. This is a most astonishing statement and needs to be confirmed.
The fossil occurs together with Durania affilanensis and Sahinia. No Hip-
purites have been found here (Parona, 1908, p. 302). Orbitoides h found
in a layer which directly overlies another with Orbitolina! So apparendy,
there are some complications at this locality. It will have to be investigated,
whether the fossil in question actually occurs in the layer with Orbitoids,
and whether it is really an Ichthjosarcolites.

Species wrongly placed into the genus:
/. ensis Pocta 1886.
*1869 (Caprinella triangularis) FriC, A. — Archiv d. natw. Landesdurch-
forschung v. Böhmen, 1, p. 199.
1886 (Ichthjosarcolithes ensis) PoCta, F. — Sitzber. k. böhm. Ges. Wiss.,
pp. (197), 207.

Pl. 5, ff. 4 ab ; PI. 6, ff. 8 ab, 9 ab 22).
(1909 Fricî, a. — Sitzb. k. böhm. Ges. Wiss., Math.-Natw. Cl., 5th. paper,
p. 2, 3.

This animal has a distinct ligamental groove on the exterior and inter-
nally three distinct cavities. Apparently no Ichthjosarcolites.

quot;) There is no reference to the figure of Pl. 5 in PoCta's text. It is also overlooked in Kühn's Catalogue.
Pl. 5, figs. 5ab depict a: „PSteinkem von Ichthjosarcolithesquot;, a most problematic piece.

Caprinella depr^sa Cotmlh i Chiozza 1851, Giornale LR. 1st. Lombardo
sc lett. arte e bibl it., 3, pp. 37, 45 ; PI. 3, ff. 8ab23) _

1892 Futterer, K.-Pal. Abh. Dames amp; Kayser, (n. f.) 2, 1, pp. 105 106
Marginal canal-walls bifurcating. Apparently no Ichthjosarcolitel.

1888 Douvillé, H. - B. S. g. F., (3) 16, p. 706 : to Plagioptjchus.
898 Douville, H. _ B. S. g. F., (3) 26, pp. 147, 150:
898 Douville, H. - B. S. g. F., (3) 26, p. 388 :nbsp;Schiosia.

A con^cise compilation from literature of the features of this genus will
be given here for further reference.

Biology: Living m groups (d'Orbigny 1850, p. 190) ; possibly free-
living, when adult; left valve always free (Fischer 1887, p. 1057)

Exterior: Inaequivalve. Right valve curved or loosely coiled, with the
turns not touching one another (Deshayes 1825, p. 499) 24) Reaching
great size. Strongly carinate. The two carinae of hicarinatus, and two of
the three of tricarinatus are regarded as siphonal ribs by Parona (1921
p. 10). The largest flange-like carina of triangularis is found on the outer
curve. Surface smooth with faint growth lines (d'Orbigny, Gemmellaro,
I arona), and longitudinal striae (Parona 1921, p. 12) corresponding to
the spaces between canals. Left valve curved in the same direction as the
right one (cf note 12), shorter.

Interior : Body cavity subcircular, oval or subquadrangular. Mould
sometimes with a depression at the concave side (Desmarest; Deshayes
1825, p. 500), or with two ridges corresponding to the carinate ribs (hicari-
natus, trtcarmatus, Parona, textff. 7, 8)^5) ; these ridges are found on the
concave side in tricarinatus. Body cavity traversing the entire length of the

shell; crossed by numerous oblique tabulae, which slope away from the
commissure towards the convex side in the right valve ; in the left, they
slope away from the commissure towards the concave side 27). As a result
the tabulae of one valve are more or less parallel to those of the other.
They are often regularly spaced, occasionally not (Deshayes 1825, p. 499).
The last „logequot; larger than the others (Deshayes 1825, p. 500)2»).

Dentition : cardinal apparatus Biradiolites-Yikt (Douvillé 1904, p. 525),
synodont; myocardinal lamina sliding in notches in the body-cavity's wall.
There are two dorsal accessory cavities, according to Douvillé (1887,
p. 793) 29). Muscles born upon the external face of the myophores (Douvillé
1888, p. 728). Teeth notched (Parona 1921, p. 9). No ligamental furrow
on the outer surface (Parona 1921, p. 9). No internal ligament either ^o).
A septum has been observed in the right valve of a triangularis from Tri-
politania (Parona 1921, p. 11) and that of a hicarinatus from Gargano
(Parona, p. 12 ; textf 10) ^i).

Structure ^2) : Entire shell-wall consisting of one layer only the
inner shell-layer (Douvillé 1904, p. 525 ; idem in litt. in Trechmann,
1924, Geol. Mag., 61, p. 400). The shell of both valves (d'Orbigny 1847,
p. 263) traversed by irregularly distributed, rounded, capillary tubules
These canals are not tabulated! (Deshayes 1825, p. 500). Specialized,
radially stretched canals have been figured by Parona 1921, textff. 7, 8, 11,
right valves. Larger canals or cavities have been observed in several in-
stances : triangularis : right valve : one large canal at the convex side („dor-

quot;) They do not turn back again, as is drawn in Woodward's fig. 16. For an affirmation of the above
description see also: Defrance 1821, Glossopètre, p. 72.

quot;) Paquier 1905, p. 94: „ .. et le point bas de leur surface (tabulae of the left valve) se trouve, comme
chez ƒ. triangularis au voisinage du bord dorsal (meaning the inner curve)quot;. There are, however, no data
about the tabulae in the left valve of the type species, and in the right valve they slope just the other way
down, if the valves arc taken apart, i. e. their lowest point there is near the convex side. If the two valves
are kept together this holds also for the tabulae in the left valve of Paquier's species. So the statement
cited is a little cryptic.

quot;) This is not so in Paquier's specimen of PI. 9, fig. 7. This may have been accidental, if the animal
had not yet reached the adult stage.

quot;) It is possible, that d'ORBiGNY 1850, p. 189 refers to a similar feature: „L'intérieur de la coquille
représente un cône arqué, quelquefois simple, d'autre fois pourvu d'un autre petit compartiment parallèle,
irrégulier, placé soit en dedans, soit en dehors,.. quot;. It is not clear, whether the words after „parallèlequot; still
refer to the additional cone or again to the mould itself, as do the words following next: „divisée sur toute
sa longueur par des cloisons ..quot;.

»») cf. Douvillé 1888, p. 728, note; the same 1904, p. 525; the same in litt. in Trechmann 1924, Geol.
Mag., 61, p. 400. An external ligamental groove was thought to exist by Stoliczka 1871, Pal. Ind. (6),
Cret., 3, p. 233: „with a ligamental furrow on the convex sidequot;. I have not succeeded in finding the source of
this astonishing statement. A „rainure ligamentairequot; upon the mould was mentioned by Douvillé in 1887
(p. 793) and by Parona (1921, p. 9; textfF. 8, 9; PI. 4, f, lb). The L of Parona's textfigure 8 can better be
regarded as the rudiment of tooth 3, and in this way might also be explained the slit on the mould. So it
is considered best to adopt Douvillé's ultimate opinion.

quot;) Parona (1921, p. 12) takes it for a cardinal septum. Some alternative hypotheses, however, are
possible. First, it might be regarded as a muscle lamina (cf. pp. 102, 103). Secondly, a similar septum was
observed in Radiolites styriaeus by Klingiiardt, F. (Die Rudisten, 1921, pt. 4, PI. 21, f. 4; 1922, pt. 2,
p. 27; PI. 3, f. 11 (same fig.)). Klingiiardt regards this septum as a sort of partition between the body
itself and the Kiemenraum.

*') The type description says on this point : „ .. encroûté vers sa pointe, d'une substance calcaire épaisse,
présentant des stries longitudinales et qui ressemble beaucoup au test des hippuritesquot;.

quot;) The „sottilissime strato interno liscioquot; of Parona (1921, p. 9) seems not to have a distinct, differ-
entiated structure.

sdquot;) and a bundle of others at the concave side „forming a depressionquot;
(Deshayes 1825 p. 500) ; „quelques autres bien plus gros Lrauxquot; r^^ •

1850 p. 192 ; PL 542, f. 3) ; some large rounded canals at the convex side
( angle ventralquot;) (Douvillé 1887 p. 793) ; subquadrangular larger canals
at the posterior side, the side of attachmentquot; (vide : orientation) near to
^ cavity ^RONA 1921, p. II). Left valve : larger, subquadrangular
canals outside the muscle laminae (Douvillé 1887, p. 793 - textf 16 •
„cavités accessoiresquot;. The description does not fit well to the figure) -'idem
at the concave side, more numerous there, than in the right valve (pIrona
oofi'nbsp;accessory cavities outside the myophores (Parona

the fossil is immaterial ^5). in /. tricarinatus the dorsal part lies on the convex

About the orientation of triangularis exists considerable controversy
From Douville's fig^l6 (1887) it appears, that the anterior side corresponds
to the inner curve. To judge from Parona's PI. 5, f. lb and textf. 9 on
the contrary, the posterior side would be found on the concave side
This agam is contradicted by Parona's text, p. 11, where he considers
the posterior side the face of attachment, which would be impossible
If It were situated on the inner curve. Douvillé's fig. 16, again, shows

that the french author considers the anterio-ventral side to be plane of
attachment.nbsp;^

This illustrates how extremely little is Imown about one of the earliest
known Rudists.

'' compared with Rousselia by Douvillé
1898, B. S. g. F (3) 26, p. 152, and in 1904, p. 525 ; with Titanosarcolites

1924 Geol Mag., 61, p. 400 ; with Immanitas by Palmer 1928, Occ Pap
Cahf Ac. Sc., 14, p. 29 (incorrectly).nbsp;P'

It is confused with Caprinula by Sharpe, 1850, Quart. Journ. 6-
Woodward 1855 Quart. Journ., 11 ; Gemmellaro 1865 ; Fischer 1887 ,'
Roemer 1888, Pal. Abh., 4, 4 ; and by Zittel, Handb. d. Pal.

L anguis-^o^t 1888, vide p. 134 : Caprinula anguis (Roemer) Douvillé
= ? Capnnuloidea anguis (Roemer) (cf. p. 137).

quot;d^f^^lquot; ..dos de la coquille» (p. 500) is meant the outer curve Paouier
1905: the mner curve is regarded as the dorsal side, apparently from'analogy with the Ca^ids

I. coraloidea (Hall amp; Meek)
1856 (Caprinella c) Hall, J. amp; Meek, F. B., Mem. Am. Ac. Arts amp; Sc.,

(n. s.) 5, 2, pp. 380, 381 ; Pl. 1, figs. 3a-f (in the text erroneously:
Pl. 2) 36).

Age : „Upper part of division No. 4 of Sectionquot; (Cenomanian in
Kutassy, Foss. Cat., 68, p. 177).

This species is insufficiendy known. It certainly does not belong to
the genus Ichthjosarcolites as the „prismsquot; are tabulated (cf, p. 55). It is
not clear whether the tabulae of one „prismquot; are independent of those of
the adjoining „prismsquot;, or whether they are arranged in funnel-plates.
In the latter case the form would belong to the Radiolitinae, in the first, it
would be some form related to those described below. The general appear-
ance of this fossil seems rather to favour the first. On the convex side
of the mould a depression is seen which one might be inclined to take for
the impression of a ligamental inflection. It might, however, as well be the
mark upon the mould of a bulging of the shell-wall corresponding to the
posterior muscle attachment area, such as occurs in Titanosarcolites.

/. coraloidea? (Hall amp; Meek)
1926 (Caprinella coraloidea?) Wade, B., U. S. geol. Surv., Prof Pap., 137,

The figures given by Wade may well represent a Radiolitid shell-
fragment. The fossil cannot belong to Ichthjosarcolites because of the trans-
verse walls in the „prismsquot;. If Hall amp; Meek's species belongs to the
Cenomanian, its occurrence in the Ripleyan is not very probable. Note,
however, the next item.

I. sp. aff. coraloidea (Hall amp; Meek)
1928 (Caprinella sp. aff. coraloidea) Adkins, W. S., Univ. Texas Bull.,

Age: Austin Chalk (Coniacian to Lower Santonian, according to
Muir, J. M., 1936, Am. Assoc. Petr. Geol., pp. 20/21).

Loc.: Travis County, Richard Schmidt quarry, near Pilot Knob,
No description. Texas.

ƒ. cornutis Tuomey
1854 (Ichthjosarcolites (Caprinella) cornutis) Tuomey, M., Proc. Ac. Nat. Sc.

. quot;) The date of this paper is not 1854 as in Kutassy, A., Foss. Cat., 68, p. 177, but 1856, according to
Marcou, J., 1885, Bull. U. S. Nat. Mus., 30, p. 13. It was communicated in 1854, but not published till
1856.

L ? (Caprlna) crassifibra (Roemer) in Scott, vide p. 131 : Catrina
crassifibra.nbsp;^nbsp;y^ujjunu

I. (Caprina) guadalupae (Roemer) in Scott, vide p. 131: Catrina
guadalupae.nbsp;^

1854 (Ichthjosarcolites (Caprinella) loricatis) Tuomey, M., Proc. Ac Nat Sc
Philadelphia, 7, p. 172.nbsp;• • .

/.? (Caprina) occidentalis (Conrad) in Scott, vide pp 131 132 137-
Caprma occidentalis Conrad and Caprinuloidea whitei (Boehm). '

I. cf occidentalis (Whitfield) in Boese 1901, vide p. 82: ? AntiUo-
caprina ? occidentalis (Whitfield).nbsp;^ ^^nmio

1854 (Ichtlyosarcolites (Caprinella) quadrangularis) Tuomey, M., Proc. Ac. Nat
Sc. Philadelphia, 7, p. 172.

1897nbsp;(Caprinella quadrangularis) Whitfield, R. P., Bull. Am Mus Nat
Hist., 9, p. 193; PI. 12, f. 5; 14, ff. 4, 5.nbsp;'

1898nbsp;(C.q.) Douvillé, H., Rev. crit. Paléoz., 2, 3, p. 123.
Age: Maestrichtian.

Its description is not up to modern demands. Most probably it is related to
Antillocaprina (vide p. 83).

/. sp. in SANCHEZ, M., 1926, Mem. Soc. Felipe Poey, 7, p. 100; PI. 8.
= Parastroma guitarti (Palmer).

1890 (Ichthyosarcolites'?) Heilprin, A., Proc. Ac. Nat. Sc. Philadelphia,
pp. 462, 469; PI. 12, ff. 2—5.38)
Age: Cerro de Escamela limestone.
Loc.: Cerro de Escamela, Orizaba, Vera Cruz.
A Caprinid with polygonal canals, as can be seen on PI. 12, f. 2.
Possibly a Caprinuloidea (cf. p. 138: ^Caprinuloidea sp.).

The „Caprinellaquot; of the Jamaican report of Sawkins-Etheridge, pro-
bably refers to TitanosarcoUtes.

pt. 4, Paléontologie, Moll, foss., p. 249.
1904 (P.) Douvillé, H. — B. S. g. F., (4) 4, p. 520.
1922 (P.) Harris, G. D. amp; Hodson, F. — Palaeontogr. Am., 1,3, p. 130.

1933nbsp;(Trechmannella nov. nom.) Cox, L. R. — Proc. Geol. Assoc., 44,
pt. 4, p. 388.

1934nbsp;(T.) Cox, L. R. — Proc. Malac. Soc., 21, pt. I, March, 1934, pp.
42—66; 27 textff.; Pis. 4—8.

*1904 (Polyptychus Morgani) Douvillé, H. — in de Morgan, loc. cit.
p. 249; PI. 33bis.

1904 (Pol.M.) Douvillé, H.—B.S.g.F., (4) 4, pp. 520—524; textff 1,2.
1934 Trechmannella morgani) Cox, L. R. — loc. cit., pp. 63, 64; PI. 8,
2 figs.

1929 (Praeradiolites (?) leesi, corrected by its author in the repdnts into
Polyptychus I.) Kuhn, O. — Ann. Nath. Mus. Wien, 43, p. 30; PI. 2,
f 1; 3, f. 1.

*') It is not dear, whether this paper appeared in 1890 or 1891. Kühn, Foss. Cat., 54, p. 20 gives 1890,
KirrASSY, idem, 68, p. 13: 1891.

1935 q Trechmannell^^^ Mac Gillavry, H. J. _ Proc. K. Ak. Wet. Amster-
dam, Jö, 5, pp. 564, 565.

1933nbsp;(Trechmannella n. sp.) Cox, L. R. - Proc. Geol. Assoc. 44 pt 4
p. 382, textf. 44 (9).nbsp;' ' ^ '

1934nbsp;(T.persica) Cox, L. R. — Proc. Malac. Soc., 21, pt. 1 March pn
43-62; textff. 1-27; Pis. 4-7.nbsp;'

1910 (Polyptjchus striatus) Douvillé, H. — Mém. S. g. F Pal 18 fasc 1
Mém. 41, p. 78; Pl. 7, ff. 1, 2.nbsp;^ iai., lö, tasc. 1,

1934 (T striata) Cox,L.R. _ Proc. Malac. Soc., 21, pt. 1, March, pp. 55,
? Trechmannella

(1930 (?Poljptychus) Adkins, W. S. - Buil. Univ. Texas, 3001 p 77
No description.nbsp;'

*1877 (Monopleurajalgasi) Vidal, L. M. - Bol. Comis. Mapa Geol. Espana
Madrid, 4, 2, p. 94; PL 2^, f. 3.nbsp;^ '

1932 Astre, G. — Buil. Soc. hist. nat. Toulouse, 64, 1, pp. 86, 87 fa
Polyptychus or Rousselia, probably a Rousselia).
Vide p. 61 : Rousselia.

Age of the genus: Maestrichtian (boundary between Campanian
and Maestrichtian, cf Cox 1934, Lc., pp. 62, 63).

Distribution: Persia (1, 4, 5), Eastern Arabia (2, 3), (? Texas
? Pyrenees). The species from Eastern Arabia have not been differendated
as yet from those of Persia.

ot the radial canals occurring in the inner shell layer of the left valve can be

between the (tangendal) sections and the radial direction of the canal's
section.

Large forms; Left valve rather low, concave side dorsal; Right valve
bent a littie in the opposite direction, (i.e. concave side ventro-posterior).

large, tapering, with two ribs on the concave side, which probably represent
the two siphonal zones. In a transverse section An directed radially, Pjv
parallel to the living chamber, at least as near to it as the anterior tooth,
pressed as it were against this cavity by the interior position of the liga-
mental rudiment. This is a rather large cavity, sometimes with a cone in
the centre. Anterior muscle area of the left valve rather steeply elevated,
separated from outer margin by a depression, and bearing the muscle upon
its exterior face; the posterior muscle area of the same valve, a raised myo-
phorous apophysis, which fits tooth-like, into an alveole of the right valve.
The muscle is thought to be inserted on the inner face of this apophysis.
Muscular apophyses conjoined with the central side of the base of the teeth
into the beginning of a myo-cardinal lamina. Outer shell-layer present,
fibrous, well developed. The siphonal ribs consist of this layer only. Left
valve with narrow radial canals, separated from one another by polyfur-
cating walls. Right valve with many large polygonal canals, that are always
crossed by tabulae, probably; this at least holds for the type species. No
specialized marginal canals. The canal-walls were probably thickened secon-
darily, during life, by the animal.

Age: Maestrichtian (cf Douvillé 1904, B. S. g. F., (4) 4, p. 524 ;
nec Campanian as in Kutassy, Foss. Cat., 68, p. 165 : the term „Cam-
panien supérieurquot;, used by Douvillé in 1898 is identical with his „Maes-
trichtienquot; of 1904 ; cf Douvillé, H., 1894, Mém. S. g. F., 4 (Mém. 6),
p. 96 and A. de Grossouvre, 1904, B. S. g. F., (4) 4, pp. 513, 514, where
this use of the term „Campanien supérieurquot; is obvious).

Monopleura (?) Jalgasi Vidal 1877.
*1877 (Monopleurafalgasi) Vidal, L. M. — Bol. Comis. Mapa Geol. Espana,
Madrid, 4 (2), pp. 350, 351 (94, 95 of the memoir); PI. 2a, fig. 3.

1932 (Monopleura (?) Jalgasi) Astre, G. — Bull. Soc. Hist. nat. Toulouse
67, 2e trim., (30 Juin), pp. 86, 87.

Astre : „11 semble qu'il faille plutôt penser à un Polyptjchus ou mieux
à un Rousselia, qui, etc.quot; ; „L'assimilation à Rousselia paraît donc très
probable . . .quot;

Monopleura(?)figolma Vidal 1877.
*1877 (Monopkura figolina) Vidal, L. M. _ loc. cit., p. 351 (95 of the
memoir); PI. 7a, fig. 3.

These forms from the Catalonian side of the Pyrenees, Maestrichtian.
The genus has not been recorded from the New-World.

Right valve straight, conical ; left valve rather strongly convex. General
appearance like a Monopkura f). An very great, near to the body cavity
gemculated, with the convex side facing the 3' alveole. Pjv rather small'
near to the edge, also a little geniculated, parallel to the anterior tooth'
Muscles attached to thickenings of the shell in the left valve, that are obli-
quely raised above the plane of commissure. No ligamental' cavity found
nor an external groove. Outer shell layer present, thin, darker than the
rest of the shell, fibrous. Left valve without any specialized structure right
valve with many rounded, tabulated canals, that manifest themselves upon
the labrum as polygonal alveoles. The canals become more polygonal
towards the dorsal side. Marginal, radially stretched canals present.

Occasionally the canal-walls seem to be secondarily thickened by the
animal during life,

Both valves possess numerous small polygonal, more or less tabulated
canals and a single row of small elongate-oval to subpyriform marginal
canals. The adjacent polygonal canals occasionally are a little radially elong-
ated. The marginal canals if tabulated at all are only distantly so.

Cardinal apparatus Monopleurid. The left valve with two notched
teeth, the socket for the equally notched tooth 5 lying between them. This
socket is not extended as an accessory cavity and consequently no septum
exists in the left valve. The entire cardinal apparatus symmetrically arranged
with regard to the curvature of the shell and the circumference of the section,
and without the Caprinid twist. The polygonal tubules invade the hinge'
teeth (especially visible in tooth and the entire area of muscle attachment
down to the body cavity.

t) It is not clear, whether this implies, that the left valve is curved towards the dorsal side.

Muscle attachment probably superficial, nearly in the plane of the
commissure (cf. p. 67).

Ligament entirely internal, wholly enveloped by the canals of the inner
shell layer, without any connection whatever with the exterior. Nothing is
revealed of its presence on the surface. It has a comma-shaped section
with both ends drawn out in a peculiar way i).

The valves are of varying shape, the left valve as a rule more curved
than the right one, curved or coiled, not always in the median plane, but
always with the inner curve and thus the umbo at the dorsal side.

Most of these features have already been described by Trechmann,
who was the first to put the genus among the Mompleurinae, but his des-
cription failed to impress itself upon the majority of Rudistologists owing
to the lack of good figures of section and structure.

The age of the genus is Maestrichtian as even the species of the Jamaican
cretaceous shales are associated with Orbitoids (Trechmann, 1929, Geol.
Mag., 66, p. 485).

This genus seems at first sight to be related to Ichthjosarcolites, but-
several important differences exist. Unfortunately the latter genus is not
sufficiently known ; neither are all its features well described. There is much
more agreement with Rousselia. The differences and affinities of the three
genera are given in the three first columns of the table given below.

The relationship between Rousselia and Antillocaprina is evidently great,
but the absence of canals in the left valve and the absence of a ligament
in Rousselia constitute an important difference. Ichthyosarcolites has appar-
ently little in common with them both and constitutes a different branch,
evoluating earlier and incidentally further as regards the hinge. Afterwards
in the Senonian, the other genera differentiated froin the main branch,
convergent with,' but independent from Ichthyosarcolites, and probably
independently from each other as well

Antillocaprina annulata (Palmer). (PI. 1, ff. 1—3; 3, f 2; 8, ff. 1, 2,
3, 7, 9; 9, f 2, 4).

nos. 15, 16, pp. 102, 103 ; PI. 9, ff. 1—3.
1937 (Caprinula cf. annulata) Vermunt, L. W. J. — Journ. Pal. (in press).

Occurrence: Ciego de Avila (type locality), Camaguey Province,
Cuba; 5 km NNW. of San Juan y Martinez, Pinar del Rio Province, Cuba
(loc. H 774); ? 2,5 km W. of Central Caracas railway station, Santa

') N.B. in more than half of the specimens, there could be found no, or scarcely any trace of the ligament.
In the other samples it was most often dissolved, but a cavity remained, retaining its characteristic shape.
Especially in the left valves only dubious traces of the ligament could be found, and its presence in that
valve could not be established beyond doubt.

Antillocaprina cannot have directly developed from Rousselia, because of the absence of a ligament
in that genus. Owing to the absence of canals in Rousselia's left valve, it is not probable, that that genus
descended from Antillocaprina.

Table showing relations and differences of American forms compared with Rousselia and Ichthjosarcolites.

Biradiolites-]ikamp;
situated in living
chamber, sliding in
notches
teeth longitudinally

canals not tabulated
marginal canals pre-
sent, reduced
both valves occasion-
ally with special-
ized canals, lacunae
or cavities,
left valve with cavities
outside myophores
no outer shell layer

rounded to polygonal
canals in right valve
only,
canals tabulated
marginal canals in

idem in both valves

idem

idem, reduced
longitudinal tubes

idem

concave side: ?
strong, sharp, carin-
ate ribs
concave side dorsal
no ribs, or rounded
to more or less
sharp ribs

Clara Prov., Cuba (loc. H55); ?? Arroyo Hondo, Camaguey Province,
Cuba (see p. 82).

62 specimens from the type locality (Ciego de Avila), most of these
received by courtesy of the Bataafsche Petroleum Maatschappij, collected
by Dr. Tschopp, and some given by Dr. Palmer. Right valves 4/3 as
numerous as left ones.

Two bivalve specimens from San Juan y Martinez, Pinar del Rio
Province. One collected by Dr. Tschopp (W 72), the other by us (loc.
H774, W7I).

Most specimens are badly recrystallized, but some are quite useful.
There can be no doubt about their belonging to Palmer's species, or to
Trechmann's genus.

Inaequivalve, right valve elongately conical, straight, cornucopia-
shaped, or more or less curved, but not to the same extent as the left valve.
Left valve with the form of a phrygian cap, occasionally capuliform, never
as coiled as some of the left valves of A. occidentalism nor involute or touching
its own commissure. Young specimens may be aequivalve, with both valves
equally curved (W 72, length ± 50, diameter 60 x 40 mm), but often very
young right valves are straightly conical (for instance Ca 58, diameter
14 mm!). Some of the latter are fixed upon older specimens of their kind,
either parallel to these, or at right angles to their surface. Probably the
aequivalve samples were either fixed to a small loose object, or actually
free-living. Commissural angle about 110°.

The largest specimen, Ca 53, a fragment of a right valve, measures
240 mm, 280 along the outer curve, with a diameter of 110 X 130 mm,
but this is an exceptionally large sample. The second largest (Ca 26) is
170 mm, 190 along the outer curve, diameter 80 X 100. The largest left
valve, Ca 16, measures 110 mm, 160 along the outer curve, diameter 80 X
65 mm. Generally the right valve must have been the larger of the two.
In accordance with this, the left valve expands more rapidly than the right
valve, the growth angle of a left valve being roughly 45° (proximo-distad),
that of a right one 30°, with a variability of 35—75° and 5—45° respectively.
The angle diminishes with age. The dorsal side is always the concave side,
and this also holds for the nearly straight right valves.

At varying intervals growth stages occur on the outer surface of both
valves. Here the outer surface and the canals bend sharply inward, then
gradually grow outward again towards the commissure, until the next
growth stage is reached. This inward curvature affects only a few outer
rows of canals. The growth stages are only lacking in a few young right
valves of the straight-cone variety.

On the convex side of the left valve often a longitudinal depression
of varying depth is present. Sometimes it is a distinct but shallow groove,
sometimes a mere flattening of the shell, more to be felt than to be seen.

sometimes entirely absent. A corresponding depression of equal variability
s found on the right valve but here on the whole it is still ll pronounced
In a few cases the depression is bordered posteriorly by a more or less
distmct rib or angularity Then, posteriorly of this rib, a very slight nearly
imaginary flattemng of the shell-surface may be present. TUs is situated
near the end of the posterior muscle impression area, the rib at the very
tip of It. So It stands to reason, that the first-mentioned depression corres-
ponds_ to the inhalent siphonal band, the rib to the „interbandequot; the
flattemng to the exhalent siphonal band. Corresponding features are found
in the species A, occidentalis and pugnijormis, but much more pronounced

Ligament as described for the genus. The extreme and aberrant special-
ization of the AntiUocaprina ligament is unique amongst Rudists and is only
parallelled by that of the pillars of Parastroma. There is no space left for
an elastic ligament. Besides, the internal position of the ligament right
amongst the mobile elements of the hinge, together with the breadth of
comn^ssure lymg dorsad of it, would preclude its being near the hinge
axis. So if there really were an elastic ligament, connecting the two valves
it would have to stretch enormously. Apparently the elastic ligament was
entirely lost and the present calcareous infolding is a mere mdiment A
similar position of the ligament is reached in the Caprinids, where, however
It is apparently always still connected with the exterior. As the ligament
m that case is a cavity, there would be room for an elastic ligament Even
abovV')''''^ probable, that there was any, for the same reasons as given

The Hgament has a fibrous calcitic structure, which must be regarded
as outer shell layer material. These fibres cross the entire width of the
ligament, i. e. the ligament is made up by one layer only, so that it has
not the nature of a true outer shell layer infolding. The fibres are crossed
by taint concentrical growth-lines.

The shape and relative position of the hinge elements can best be
judged from the photographs and accompanying diagrams. The tooth
alveoles Aij and Pjy' are unequal. Aj/ has an oval section, pointed
towards the living chamber. The Pjy' has a more irregular outline with
the greatest length parallel to the body cavity circumference, its anterior tip
curled around the ligament. The two teeth lie very close together, sometimes
nearly contiguous. They must have been nearly straight, but for the cur-
vature of the growth direction. Their length cannot have been very great •
in Ca 28 (length 60, diameter 63 mm) it cannot exceed 10 mm, the distance
between the commissure and a section. The outlines of all three alveoles are

») For a similar reasoning with regard to Trechmannella vide Douvillé, H., 1904, B. S. g. F (4) 4 n 521 ■

W^Sr T '^PP^'^eil cardmal et le grand développement des canaux qui séparent cet appareU
ItreTa d^n marT I ^nbsp;^ Pl^^i'^quot;« reprises que l'arête cardinale jouait e rôle dŒ

distinctly undulated, so that the teeth must have been longitudinally notched
or ribbed, tooth 3 especially on the posterior side. The alveoles A// andP/^
are separated from the body cavity by a small strip of the inner shell layer,
about 4 canals thick in a large specimen (Ca 54). The consequences of the
curious fact, that the tooth 3 lies more to the exterior than the ligament,
have already been discussed above. Everything else, including the way in
which the posterior tooth curls round the ligament, is the logical sequel
of the latter's emancipation towards the interior. The Antillocaprina hinge
can be derived directly in this way from that of Monopleura michaillensis
Pictet-Campiche for instance (cf Douvillé 1936, B.S. § F., (5) 5, fig. 10b).

The nature of the muscle attachment could not precisely be ascertained.
I have had a longitudinal section made through the few commissures there
are in the collection, but none of these have yielded any evidence. It may
safely be inferred from Palmer's PI. 9, fig. 3 and from the nature of the
muscle attachment of A. occidentalis (cf Whitfield PI. 16, fig. 4, ma,
left valve; Trechmann, PI. 25, fig. 2, ma, tight valve), that at least the
anterior muscle attachment was superficial, nearly in the plane of the com-
missure, bounded exteriorly by a shallow marginal depression in both
valves. The posterior muscle attachment area, in sections, is a little larger
than the anterior one. Its nature is not so clear as that of the anterior muscle
area. According to Palmer, it is „linealquot;. This is not in accordance with
my observations in the sections, where it seems to have a distinct breadth.
The posterior muscle insertion of A. occidentalis is not clear either (Whit-
field, PI. 16, f 4), but it is certainly not tooth-like, as in TitanosarcoUtes
(see pp. 87, 88).

The body cavity traverses the length of both valves and is subdivided
by coarse tabulae, which correspond more or less to the growth layers on
the extetior. These tabulae are plane in the left valve, but cupped in the
right valve, with the concave side facing the aperture Sometimes the
latter have a sharp downward point in the centre, somedmes they are steeply
conical. Occasionally a new tabula in the right valve is affixed to the one
below.

Tabulae occur also in the tooth alveoles. The living chamber has a
subcircular or elliptical section, with the long axis directed either from the
posterior tooth towards the antetio-ventral side, or transverse, i. e.
proximo-distad. The shell-wall is always thickest at the dorsal side, so that
as a whole the body cavity is excentrical towards the ventral side. Acces-
sory cavities do not exist, but sometimes in the cardinal region the shell
substance has been dissolved and small calcite-rhomboeder geodes have
formed. This may also be the case with both muscle area's.

♦) The tabulae that cross the canals of Sabitiia totiseptata show an analogous disposition, cf. Palmer
(1928, Occ. Pap. Calif. Ac. Sc., 14, p. 73): „The septa in the canals of the lower valve are concave and those
in the upper valve are flat.quot;

Fig. 1. AntiUocaprina annulata (Palmer), juvenilis (Ca58. diameter 14 mm); drawn after the section
figured on PI. 9, f. 4. Showing the oval section of the marginal canals in a young specimen, the canali-
culi that cross the canal-waUs up to the median line, and the peculiar structure that may represent
the outer sheU-layer, forming minute longitudinal riblets. On top of the riblets is found a Biradiolites
sp., with one of the funnel-plates drawn in. X 34.

Fig. 2. Antilhcaprina annulata {0.2.1, diameter 55). Older stage with longer marignal canals. Note
canalicuh and median plane. The specimen is grown upon by a strange organism, but was weathered
down to the marginal canals before that. In the canals are observed calcareous laminae, shutting off
the inner part of the canals. Possibly the specimen was worn down during life, and the calcareous
laminae are a regenerative phenomenon (cf. p. 72, note 6). X 34.

Fig. 3. AntiUocaprina annulata (Ca54, diameter ± 80), drawn after the section, figured on PI. 8,
f. 9. Note position of cardinal elements and ligament. The limit between thick-waUed and thin-walled
canals is indicated by a full-drawn line. Three lines indicate, where the muscle area's and the dorsal
patch of small canals are set off sharply against the rest of the structure. One of the tabulae in the
body-cavity is plied against another. Natural size.

Fig. 4. AntiUocaprina sp., from Jamaica, in the Naturhistoriches Museum, Basel. L nearer to body
cavity than in annulata ; large thin-walled dorsal canals ; ventral and anterior rib. Natural size.

Fig. 5. AntiUocaprina pugniformis (Palmer) (Ca65). Horizontal section through left valve, with tooth
3 and its alveole. The full-drawn line limits the marginal canals. Natural size.

Fig. 6. AntiUocaprina pugniformis (Ca63). Section through right valve, near the commissure. The
full-drawn line limits the marginal canal-zone. Natural size.

Fig. 7. Section through same specimen as fig. 6, 4 (dorsaUy) to 17 (ventraUy) mm lower down.
Natural size.

Fig. 8. AntiUocaprina crassitela n. sp. (W 115.2). L near to body cavity. Curvature shifted a little
towards the anterior side. Natural size.

Fig. 9. AntiUocaprina crassitela (W 115.1), drawn after the section figured on PI. 8, f. 6. A micropho-
tograph of a detail of this figure is given on PI. 9, f. 3. L near to body cavity. Irregular outline of body
cavity, curving round the myophorous area's. Natural size.

Figs. 1—4. Titanosarcolites giganteus (Whitfield) (Ca 81), four consecutive sections : 1 amp; 2 both
sides of a cut through the left valve, 3 amp; 4 both sides of a cut 5—12 mm further towards the right.
The commissure is touched at the top of fig 2, and to the right of fig. 3. Note bulging of mp area,
and the tooth-like nature of the posterior myophore. The ligament is visible in fig. 4. Note presence
of posterio-ventral ribs, probably a siphonal feature. Natural size.

Fig. 5. Titanosarcolites giganteus (Ca 70). Note siphonal area, and slight bulge near the mp area, x 0,6.

Fig. 6. Titanosarcolites giganteus, drawn after Whitfield's PI. 21. The figure has been reversed to
bring it in the usual orientation. Whitfield's tabulated lt;7, a cavities arc the tooth alveoles, ma area
distinctly visible. Note anterio-dorsal belt of tubes. X 0,5.

Fig. 7. Titanosarcolites giganteus (S 65). Siphonal area with nearly occluded grooves. Natural size.

Fig. 8. Antillocaprinae aff genus B. (W 132) with Orbitoids. Note flange-like ribs. X 0,7.

Fig. 9. Detail of the section figured in fig. 8 (indicated by dotted line), showing peculiar submarginal
canals, constricted by ridges. X 14.

Fig. 10. Titanosarcolites giganteus, aberrant tubes (a, d, e, f: Ca 83 ; b : S 69 ; c : Whitfield's PI. 21).
The arrow points towards the exterior. Natural size.

Fig. 11. Titanosarcolites giganteus {Ca77), a 27 mm above b, showing the growing over of a tube,
and the subsequent formation of new ribs. Natural size.

Trechmann mentions the existence of an outer shell layer in other species
of this genus. In not a single specimen of A. annulata could such a layer be
found, not even underneath the Rudists attached to them. It must be stated,
however, that the Antillocaprinae are frequently worn down to the marginal
canals even underneath the attached small Rudists. So apparently they were
already eroded before being grown upon. In accordance with this, the attached
Rudists grow in different directions, giving evidence that the Antillocaprinae
were lying, some upon their anterior, others upon their dorsal or posterior
side, and others again standing upright. So one gets the impression, that
several of them had been thrown about before they were grown upon, but
we cannot be sure, because we do not know, whether they had any fixed
position during life. In any case, they were not all just lying around dead
at the time, for some are grown upon by young specimens of their own
kind. Only in Ca 58, an extremely young right valve (diameter 14 mm)
attached to Ca48, a structure is found, forming a series of riblets, that
might be taken for the outer shell-layer (PI. 1, f 1; 9, f. 4). If so, it is so
extremely thin, that it would not be surprising, if indeed it wore already
off after a short time.

The canals of the inner shell layer can be best observed in a large right
valve (Ca 54; PI. 8, f. 9), on which the following description is largely based,
checked and completed by observations from other samples. The sub-
pyriform canals of the marginal row have thick walls and no transverse
tabulae. The original fibrous structure of the walls is sometimes preserved.
The fibres radiate outwards from the canal's lumen. Occasionally minute
canaliculi are observed running in the same direction, but as these do not
pass through the entire thickness of the wall, they may be considered
to be mere constructional flaws (Ca 58; PI. 1, £ 1; 9, £ 4).

a)nbsp;A few rows, adjacent to the marginal row of canals, are like these,
in being thickwalled and devoid of transverse tabulae. Only once have I
observed a concave tabula in one of these canals (Ca 20). Their lumen is
more or less rounded, their diameter up to 1 mm or a little more. The walls
of these canals are double, as well as those of the marginal ones, presenting
down the middle a dark median plane. The two parts on both sides of
this plane are darkish hyaline, with an occasional concentrical growth line
here and there, showing that the walls were secondarily thickened by the
animal

b)nbsp;Adjacent to the thick-walled polygonal canals comes the bulk of
the polygonal canals. These are thin-walled and truly polygonal, and have
many transverse tabulae. Just below a growth stage, the tabulae crowd
much closer together. It stands to reason, that there is a connection between

') A similar observation has been made in Rousselia by Doiatillé (1898, B. S. g. F., (3) 26, p. 152).
On the inside of the hyaline layer of the canal-walls in Antillocaprina, one may often observe a fibrous layer,
which has the fibres radially arranged, i. e. directed towards the canal centre. They often show several
growth lines. It is possible, that this layer is of secondary origin, caused by a crystallization proccss.

the presence of tabulae in these canals and the thinness of their walls s).
Here too a dark median plane may frequently be observed running down
the middle of the walls. This is a plane of least resistance, and often in
the vicinity of a dissolved area, the walls split up along this plane, the
adjoining canals are severed, and are found swimming loosely in the'sub-
sequendy formed caldte crystals (Pl. 9, f. 2). The diameter of the thin-walled
canals is also up to 1 mm or a litde more, but they are very irregular in
size, small canals filling in the spaces between the larger ones (see below).
Moreover those situated in the area's of muscle attachment are distinctly
smaller, with a diameter of about 0,5 mm. In this way the muscle area's
are quite sharply delineated, at least at their dorsal border. Here also the
section of both the smaller canals of the muscle area and of the larger canals
surrounding it, may be distinctly lengthened parallel to this border. The
latter feature is highly reminiscent of a similar disposition of the canals in
Titanosarcolites. Dorsad of the cardinal region another area of thin-walled
0,5 mm canals occurs, sharply defined at the dorsal side, but with the canals
increasing gradually in size towards the hinge, until the normal width is
attained. The canals in the base of the tooth S are smaller still, thick-walled
and rounded. A clear differentiation of the patches with small-sized canals,
can, of course, only be present in a fairly large sample.

The limit between the two kinds of polygonal canals (thick-walled and
thin-walled) is pretty sharp, and in some specimina the thick-walled canals
only have been preserved, whilst the other ones are entirely recrystallized.

The pyriform canals of very young samples are shorter than those of
an older one but just as broad, and have a more elliptical section. The
other canals do not increase in size with age. On the contrary, in a young
sample the large canals are relatively more numerous. Thus the number
of canals in an older specimen is much greater than in a young one. It seems
probable, that the small canals that fill in the spaces between the larger
(see above) are the beginning of new canals, interpolated between those
already existing. The distribution of the largest canals in a large specimen
is highly suggestive of this. A similar fact was observed in the marginal
row of canals in a young specimen (Ca 58, right valve). There, in some
places, a lanceolate marginal canal of second rank was found, intercalated
between two adjoining subpyriform ones (PI. 1, f. 1). These also may
be considered to be the first stage of a new marginal canal.

Final considerations: The species is enormously variable in many
respects, but on the whole the disposition of the cardinal elements is very
constant, although the relative distance between An and Piv\ and the
shape of the latter may vary to some extent. The shape of the ligament
in this species and for that matter, in the entire genus is very constant.

«) The secondary thickening of the canal-walls in Rousselia and Antillocaprina, and the relation between
this thickening and the absence or scarcity of tranverse tabulae, indicates, that the canals were at least
tor a time occupied by part of the organism. In other words, filaments with the length of the distance between
tabulae must have projected from the mantle surface into these canals. Another argument for this mav
be the possible regenerative phenomenon, figured on Pl. 1, f. 2.

The species may be identical with Caprinula cuhensis Douvillé 1927, in
which case its specific name would have to be changed. It seems to resemble
the Antillocaprina (?) sp. from the cretaceous shales of Blue Mountain Peak,
Jamaica (Trechmann 1929, PI. 18, ff. 4, 5) but Trechmann's material is
not sufficiently preserved for a decision. Like A. annulata it presents growth
lines at the exterior.

Owing to the variability and in view of the insufficiency of our know-
ledge of other species it is difficult to give a specific charactedzadon. The
presence of growth stages might be considered to be only of relative value
as it might subject to the outher circumstances, but then the ableness to live
in these surroundings may be specific for all we know, and we must content
ourselves with whatever there is.

Association: In addition to other specimens of its kind, the following
species were found growing upon A. annulata at Ciego de Avila: Mitro-
caprina tschoppi (Palmer) (upon Ca 26, 56, 62), Biradiolites cf. adhaerens
(Whitfield), and a coral. Inside the body cavity of Ca 40, Camerina dickersoni
was found, which establishes its Maestrichtian age.

To this species I also refer a small lower valve (preserved only as
a section), collected 2,5 km W. from Central Caracas, Santa Clara Province,
Cuba (loc. H 55, S 99), associated with Inoceramus sp.

thickness of the walls, dorsally of the dorsal patch of
small canals:nbsp;'nbsp;0,03—0,04

') Values of this kind, are by necessity arbitrary, but they suffice to give the order of magnitude.

The corresponding values for No. 54 though they
cannot be exactly measured are mainly similar to
those of No. 40.
Thick-walled polygonal canal, absolute maximum (except-
ional), Ca 37 (diameter 27, length 32):nbsp;3 j
Distance between the tabulae of the thin-walled canals of

Size of Z., maximum (No. 25, diameter 75, length 120) 6
Distance between L and living chamber,

minimum measured (No. 40, see above, sizeZ.: 1,7): 3,6
Distance between An and Pjv

1933 (Caprinula pugniformis) Palmer, R. H. — Rev. Agric. Habana 14
nos. 15, 16, p. 102, PI. 7, ff. 3, 4.

Three specimens from the type locality, Ciego de Avila, collected by
Dr. Tschopp and Dr. Palmer. One a slightly curved and a little twisted
right valve (Ca 63), one a capuliform left valve (Ca 64), and the third a
nearly aequivalve specimen with the joined valves about equally curved
(Ca 65). All are small specimens, with a proximo-distad diameter of resp.
35, 32, 42 mm. Ca 63 has a length of ± 56 mm. The two valves of Ca 65
together measure 50 mm, ± 95 mm along the outer curve. Palmer gives
a diameter of 20—60 mm for his specimens.

») Proportional values like these are very inaccurate, so that they may be used for specific determination
only m connection with other features.nbsp;ueiermination

The species is very similar to young specimens of A. annulata and
differs only in the following respects :

S and E distinct channels, E narrower than J. / a distinct rib,
elevated, with a rounded triangular section. Anterior of E two (or 1) ribs
separated by a shallow or a deeper channel. Anterior of them another more
or less deep channel. So there are 4 (or 3) channels in all, and 3 (or 2) ribs,
or if we also count the dorsal half-ribs that bound S and the foremost chan-
nel : 5 (or 4) ribs.

The body cavity is a little larger than that of the preceding species,
the dorsal shell wall especially in the left valves is decidedly thinner, and
the tooth S lies nearer to the living chamber (distance 0,7 mm in Ca 65 ;
the strip of inner shell layer separating the alveole from the body cavity
being 0,3 mm; the distance between alveole Z' and the body cavity in
A. annulata, a specimen of the same size, is 3,3 mm (Ca 19, diam. 42 mm).

Marginal canals, if tabulated at all, only with a few scattered tabulae.
A dorsal patch of small canals is present but not as sharply delimited as in
A. annulata Ca 54, but for that matter, neither is it in a smaller sample of
that species. Between L and Piv there is only one row of canals which
is also the case in small specimens of A. annulata.

Palmer (p, 102) mentions the existence of a „capa exterior delgadaquot;
(a thin outer shell layer). It is not clear, whether there is a real outer shell
layer, or whether the outer part of the inner shell layer, formed by the
contiguous outer walls of the marginal canals is meant; cf for instance:
Palmer 1928 (Occ, Pap. Calif Ac, Sc,, 14, p. 65, on Planocaprina) : „The
outer ends of the radial plates thicken until the edges touch and then anchy-
lose forming what may be termed for convenience, the outer layer of the
shell.quot;

Association: Camerina dickersoni was found in the body cavity of
No. 2, establishing its Maestrichtian age.

idem between 3' and the living chamber:nbsp;o's
Distance^ between L and the living chamber, divided by

Hist., 9, pp. 193, 194; PL 10, f 1; 11, f. 1, (2); 12, f. 1, (3); 16, ff.' 1 -4;

(1923 (Caprinella 0.) Stanton, T. W. in Vaughan, T. W. — Journ. Washing-
ton Ac. Sc., 13, no. 14, p. 305.
1924 (Antillocaprina 0.) Trechmann, C. T. — Geol. Mas 61 o 407-
PL 25, ff. 1—3.

Occurrence: Rudist limestones of Jamaica: Logie Green (rather low
in the section, but above layers with Chiapasella radiolitiformis, Titanosarcolites
giganteus and Praebarrettia sparcilirata). Clarendon Parish; near Christianna
and elsewhere in Manchester parish; N. slope of the Great River Valley
below Catadupa. (Whitfield p. 194; Trechmann p. 407).

The species is also reported from the Island of St. Croix (Vaughan,
det. Stanton), but the specific 'determination may have to be revised now!

The descriptions of Whitfield and Trechmann may be repeated here-
Inaequivalve, right valve generally the larger. Right valve long, straight,
„slightly enrolledquot;, twisted or loosely spiral corkscrew-like, gradually
expanding from the apex outward; its surface smooth, ribbed or slightly
channeled. Left valve coiled and generally more or less involute, often
closely so, turned either towards the left or right, often nearly symmetrical.
Its surface nearly smooth or longitudinally ribbed. These ribs, from 5 to 10
in number, are elevated and distinct, rounded or subobsolete. Neither valve
with growth stages. The growth angle, especially in the left valve is distinct-
ly smaller, as a rule, than that of A. annulata.

Left valve with two sharp and bent cardinal teeth, the posterior the
larger, socket 3' lying between them (This socket may be seen on Trech-
mann's PL 25, fig. 3). Body cavity small subcentral, traversing the length
of both, valves, elliptical in section, with the longest axis from the posterior
tooth towards the ventral side, a litde anterioriy directed. In the right

valve it is strongly and distantly tabulated by very oblique, curved tabulae.
The tabulae of the left valve are very irregular, much more oblique and
generally more delicate in texture than those of the right valve; some of
them appear to extend into the central cavity as free lamellae before cutdng
off the cavity from the space below. Muscular scar ?na of left valve large,
somewhat flabellate, bounded exteriorly by an abrupt irregular marginal
depression. Such a marginal depression is also shown outside one of the
myophores of the lower valve on Trechmann's PI. 25, f 2 (presumably
the md).

Outer shell layer very thin 9). Marginal canals radially elongate-oval in
section. If tabulated at all only distantly so. The other canals polygonal
(hexagonal) or oval in section, small with occasionally a few large tubules,
generally not much more than 0,5 mm in diameter i®), divided transversely
at distances about equal to their own diameter by horizontal tabulae.

Associated with Biradiolites adhaerens, a small ?Bournonia (Whitfield,
PI. 12, f. 3: „young Radiolites macroplicatusquot;) and Actaeonella sp.

There is little foothold in this description for a specific comparison.
The most important points are the following: the coiling of the left valves,
the absence of growth stages, the aspect of the outer surface: smooth to
ribbed, the small growth angle.

The canals are evidently like those of A. annulata and different from
those of A. crassitela.

Occurrence: Catadupa, Jamaica. From the Naturhistorisches Mu-
seum in Basel, collected by P. W. Jarvis 1927. Also found in Cuba (p, 78).
Several fragments and a rather well preserved lower valve (diam. i; 50 X 70,
length (60) mm), from which the following details are taken.

The outer surface bears two disdnct ribs (I and an anterior rib). There
are no growth stages.

Rado: distance between ligament and body-cavity, divided by the size,
of the ligament, smaller than 1 1 In a section the alveole Piv much curved
at the anterior end, and rather stretched proximo-distad; its outline disdncdy
undulated at the anterior end. An indistinct but certainly smaller than
Piv'. The muscle area's could not be traced.

Between the outer surface of this specimen and the base (anterior side)
of a Bournonia growing upon it, there is a distance of 0,4—0,5 mm (PI. 1,
f. 4). This suggests the former presence of an outer shell layer. In other places,
however, the attached organisms are plied directly against the outer surface
of the Antillocaprina'^ inner shell layer. The conclusion is, that, if an outer
shell layer existed at all, its maximum thickness possible was 0,4—-0,5
mm, while at the dme it must already have been rubbed off in places.

•) Again there is no icnowing, whether there is a real outer shell layer (cf. p. 75).

The marginal canals are distinctly tabulated, with the tabulae concave
towards the commissure, or, occasionally horizontal. The tabulae are irre-
gularly spaced. Dorsally the marginal canals are reduced, but, ventrally,
they are well developed. Their walls are much thinner, than those of the
marginal canals of A. annulata, so again we have the relation between a
relative thinness of the walls and the presence of tabulae.

The cardinal apparatus is surrounded by a recrystallized patch of
calcite, sharply delimited dorsally. Dorsad of it lie large thin-walled polygonal
canals. The polygonal canals following towards the margin decrease rapidly
in size and become relatively more thick-walled. Fairly large-sized canals
occur also ventrally. The polygonal canals are horizontally and closely
tabulated, probably a little more closely so than those of A. annulata.

Association: a Bournonia sp. grows upon this sample and numerous
Camerina sp. are found in its body-cavity. Adhering to one of the fragments
was found part of what most likely is a Biradiolites adhaerens (Whitfield).

value:
Idem at the E zone:
Idem at the S zone:
Thickness of the radial walls of idem:nbsp;' 0 04

Distance between the tabulae of idem, minimum measured: 2
Polygonal canals, dorsally of the cardinal apparatus, greatest

To the same species must be reckoned two left valves from the Sierra
de Najassa, Camaguey Province, Cuba (loc. L 684; Ca 66,67 ), one of which
differs slightly through lack of ribs, and the near equality of its two teeth
(Ca 66). Both have many large canals, and generally agree in all other respects
with the Jamaican material described.

specimina, a Nerineid and Camerina dickersoni, which establishes its Maes-
trichtian age.

The Jamaican samples were collected together with several of the Rudists
described by Whitfield and Trechmann, and yet they do not fit in with
the description of the species occidentalis, because of the size of the canals,
and the presence of tabulae in the marginal canals. But for these points I
would have referred both the Catadupa and the Sierra Najassa material to
the type species. From Caprinella quadrangularis Whitfield they differ by the
shape of their section.

Antillocaprina crassitela n. .sp. (PL 1, ff. 8, 9; 8, f 6; 9, £ 3); from
crassus: coarse, tela: tissue.

Three weathered, slightly curved, right valves (W 115, 1—3; No. 1:
type specimen). This species differs from A. annulata in the following points:

All canals, except those situated in the fjip area, thick-walled, and on
the whole smaller. There are very few tabulae in the canals, and the few
present, are concave f). The cardinal elements are more or less sheathed
with a compact layer of the inner shell.

The ligament is relatively nearer to the body cavity and comparatively
larger. Piv is accordingly smaller, more jammed in between L and the
living chamber. An is relatively further away from the body cavity, and
the distance between An and Piv is greater.

The body cavity has a more irregular section, and curves round the
muscle area's (cf Titanosarcolites).

The specimens are eroded, so that not a single marginal canal is pre-
served. As a consequence of this the nature of these canals, and the features
of the exterior could not be determined. My impression is that the species
was ribbed, but of course one cannot be sure.

The cell-walls are hyaline with a distinct dark median plane. Sometimes
there is an indication of growth lines or of a two-cycle deposition.

Association: Camerina dickersoni ^^^ found in the living chamber
of No. 1, establishing its Maestrichtian age.

Canals in mp, more or less thin-walled, mean diameter: 0,6
Thickness of the walls:nbsp;0,03—0,05

t) The following relation seems to exist in the Antillocaprinlnae: the fewer the tabulae, the
more they are concave.

Distance between tooth S and the body cavity (No. 2, dia-
meter (35), length (45):nbsp;' (5)
Distance between L and the body cavity, divided by the
size of L No. 1: 1 j
No. 2: 0,7'!
Size of L, No. 1: 45

Undl the species are better known, the following table may serve to
distinguish them.

at the utmost one rib present (I). (L-CVjL = 2—4, An'-Piv' lt; 5,
body cavity small, elliptical, shell dorsally thick, the distance S'—CV

6nbsp;(7) Distinctly ribbed (4 to 5 ribs: ant., 1—2 ventr., 7, post.); left valve

capuliform. (L-CVjL = 2V2, body cavity larger, transverse, shell
dorsally thinner, the distance 3—CV much smaller than in A.

Antillocaprina cf. occidentalis.
1924 (Caprinella cf. occidentalis) Trechmann, C. T. — Geol. Mag., 61,
p. 9 ; PI. 1, f. 3.

Occurrence: Rounded off in conglomerates in the carbonaceous
shales of the Richmond formadon (lower eocene), Port Maria, (St. Mary),
Jamaica. For the age of the formation cf. Trechmann 1927, Geol. Mag.,
p. 64. The fossil is derived from the Maestrichdan Rudist limestones.

Antillocaprina (?) sp.
1927 (Antillocaprina (?) sp.) Trechmann, C. T. — Geol. Mag., 64, pp. 59,

60; PI. 2, f 10; 4, f. 6.
1929 (Antillocaprina (?) sp.) Trechmann, C. T. — Geol. Mag., 66,
p. 488 ; PI. 18, f. 6?.

Occurrence: Cretaceous shales, older than the Rudist limestones but
of Maestrichdan age (Trechmann 1929, p. 490), in the Catadupa-Cambridge
railway cutting, Jamaica (Trechmann 1927, pp. 41, 42, 59, 60); Blue
Mountain Peak, Jamaica (Trechmann 1929).

Description (after Trechmann) : Free or very lightly attached form,
nearly aequivalve right valve rather the larger and more conical (38 mm),
left valve capuliform, arched and with the spire anteriorly directed (31 mm) ;
outer layer very thin apparently smooth except for fine rather widely
spaced longitudinal ridges, crossed towards the juncdon of the valves by
fine irregularly spaced growth ridges. One specimen with the right valve
nearly as strongly arched as the left, both valves joined : 68 mm. The
specimen from the Blue Mountain Peak has a curved and inrolled oudine :
its structure is made up of long packed tubules.

Not specifically idendfiable, but different from A. occidentalis from the
cretaceous limestones at Catadupa and Logie Green.

Antillocaprina (?) sp.
1929 (Antillocaprina (?) sp.) Trechmann, C. T. — Geol. Mag., 66, pp. 487,
488 ; PI. 18, ff. 4, 5.

Occurrence: Cretaceous 300' below Blue Mountain Peak summit,
Jamaica; found together with an Orbitoid (Trechmann,p.485), and thus
of Maestrichtian age. (cf Trechmann, I.e., pp. 481, 485, 490).

Description (after Trechmann) : lower valve conical, with a smooth
outer layer with four or five prominent irregular foliated growth lines;
apex rather twisted. The specimen shows the space occupied by the median
tooth of the lower valve, and apparently the sockets of the two teeth of the
upper valve, situated near to the rather straight hinge line. The middle
layer is a mass of parallel tubules which (evidently : the walls of which)
near the margin divide up into twos or threes by the intercaladon of smaller
and shorter tubules.

Occurrence: 6 km NW. of Tranca, S\V. from Pinar del Rio, Cuba
(^loc. M940 ; W73).

A small left valve with faint indications of growth lines, but with a
dorsal shell-thickness like that of A. pugniformis.

? AntiUocaprina cuhensis (Douvillé).
1927 (Caprinula cuhensis) Douvillé, H. — B. S. g. F., (4) 27 pp 51 52
53; textf 1.nbsp;' '

Occurrence: Arroyo Hondo, Camaguey Province, Cuba.
I have a lingering doubt, that the „grands canauxquot; of Douvillé may
represent the recrystallized area of thin-walled canals of an annulata-liVt
AntiUocaprina. The form and position of the ligament, the shape and place
of the living chamber and the number of its transverse tabulae, as well as
the thickness of the shell, dorsally, are all in favour of this idea. Should
not only the generic, but also the specific approximation be correct, then
the name annulata would have to be replaced by Douvillé's name : cuhensis,
as this would then have priority.

? AntiUocaprina ? occidentalis (Whitfield).
(1926 (Caprinella Occidentalis) SAnchez y Roig, M. — Soc. geogr de Cuba
p. 11.

(1926 (Caprinella occidentalis?) Douvillé, H. — C. R. S. g. F., p. 71.
1926 (AntiUocaprina (Caprinella) aff. occidentalis) SAnchez y Roig, M. —

Mem. Soc. Felipe Poey, 7, pp. 99, 100 ; PI. 6.
1926 (? AntiUocaprina occidentalis) Douvillé, H. — B. S. g. F., (4) 26,
p. 131.

(1927 (AntiUocaprina occidentalis) Douvillé, H. — B. S. g. F., (4) 27, p. 50.
O ccurrence: Arroyo Hondo, Camaguey Province, Cuba.
Sanchez's description (1926, pp. 99, 100) starts with translations
from Whitfield and Trechmann. „No hay tabiques en la camara de
habitacion . . .quot; (p. 100) is evidently an erroneous translation for „there
is no septum^ m the living chamber . . .quot; (Trechmann, p. 407), as there
are ,,tabiquesquot; but indeed no septum in the species. The rest of the
description is very short, owing to the insufficiency of the material.

It appears to be a left valve of some AntiUocaprina or Caprinid, more
coiled still than the left valves of A. occidentalis. Entirely silicificated. Inner
features unknown. Generic determination uncertain.

? AntiUocaprina ? occidentalis (Whitfield).
(1901 (Ichthjosarcolithes cf. occidentalis Whitf) Boese, E. — Z. D. g. G., 53,
p. 178.

Boese (1901, I.e., p. 180), parallels these strata to the Texan Washita
division. Burckhardt (1930, I.e., p. 198) and Renz (1936, Abh. Schweiz.
Pal. Ges., 57, p. 2) put them into the Cenomanian, of equal age as the
Woodbine division, whereas Palmer (1928, Occ. Pap. Calif Ac. Sc., 14,
pp. 42, 47; cf Burckhardt, I.e., p. 199, note) thinks, that they partly
might be even younger still, i. e. Turonian. In any case, the formation
is too old for Antillocaprina. The most rational explanation is, that Boese
confused Whitfield's „Caprinella occidentalisquot; with Conrad's ,,Caprina
occidentalisquot;, which occurs in the Escamela limestones according to
Boehm (cf pp. 131,132), and that he substituted Caprinella by its lawful name:
Ichthyosarcolites.

The first Caprined fragment described by Thiadens (1936, Proc. K.
Ak, Wet. Amst., 39, 8, p. 1011, line 2—8) may belong to Antillocaprina,
as well as several other fragments from different localities, I will pass them
over because of the uncertainty involved. Some of them may as well belong
to the next two forms. Thiadens's fragment was found at loc. H617,
10 km E. of Fomento, Southern Santa Clara, Cuba (S 95), It is associated
with Bournonia, Orbitoides and a Nerinae.

The collections contain some curious forms, that cannot be passed
over entirely. Although their dentition is unknown and no ligament was
found, it seems safe to place them into the neighbourhood of Antillocaprina.
They have the following features in common with the rest of this group :
the general appearance of the tabulated body cavity; lack of an outer shell
layer; inner shell layer made up of many polygonal, tabulated canals. Peculiar
to them are : the presence of sharp ribs coupled with the absence of the
longitudinal tubes of Titanosarcolites.

These forms apparently occupy an intermediate position between
Antillocaprina and Titanosarcolites. In the absence, however, of any data on
the left valve's dentition, we can have no certainty.

To these genera may belong the species Caprinella quadrangularis Whit-
field 1897 and Caprinula quatuoralata Palmer 1933. Both forms have been
insufficiendy described, so that it is impossible to determine their relation
to, or possible identity with either of the Cuban forms described below.
Because of this reason, and owing to their bad preservation, the Cuban
species have not been named, even though the name quadrangularis has no
validity as it is preoccupied by Ichthyosarcolites (Caprinella) quadrangularis
Tuomey, One might perhaps suppose, that a young Titanosarcolites may
have lacked the characteristic tubes. In that case it would be much like the
form described from H 627, and come naturally under this heading.

revisional studies in rudist paleontology
Antillocaprinae aff. genus A. (loc. H 627). (PI. 1, f. 10).

1936 (Caprinidfragment) Thiadens, A. — Proc. K. Ak. Wet. Amst 39 8
p. 1011, line 13, 14; textf. 3 (14).nbsp;' ' '

(1936 (TitanosarcoUtes giganteus) Thiadens, A. — I.e., p. 1018 fpp • loc
H 627).nbsp;^nbsp;'

(1937 (?Antillocaprina) Thiadens, A. — Geogr. en Geol. Med Utrecht
No. 12, p. 43.

Occurrence: 3 km NE. of Fomento, Santa Clara Province, Cuba
(loc. H 627, S 98 amp; S 64); 4 specimens, all eroded or incomplete.'

Strongly curved, small valves with disdnct sharp dbs. Diameter 40 mm.
The ribs have a rather sharp triangular section, with a maximum height
of 10 mm. Body cavity subquadrangular in secdon, subdivided at regular
mtervals by transverse tabulae, some 9—13 mm distant inter se. The tabulae
neariy plane, but curved towards the commissure near the edge. On the
side of the inner curve in one of the specimens in a longitudinal secdon
a secondary cavity is seen, which is closely tabulated (distance between
these tabulae : 3 mm). This cavity must be one of the alveoles (or, in case
It is a left valve : the alveole). On this side, however, also some large tabul-
ated canals exist. The marginal canals are reduced, egg-shaped in secdon
pointing towards the exterior. The length of their lumen is about 0,4—
0,5 mm. The adjacent polygonal canals are of similar size; the canals'be-
coming larger towards the interior. They are irregulariy and concavely
tabulated, with the distance between tabulae generally greater than the
canal's diameter. The canal-walls vary in thickness (0,06—0,12), but are
on the whole relatively thick as compared with those of Antillocaprina
annulata. No ligament found.

Association: Lepidorhitoides (cf Thiadens, p. 1011), testifying to its
Maestrichtian age.

Observations: this fossil differs from Antillocaprina by the presence
of the sharp ribs all round the circumference, and the presence of larger
canals, both features of litde consequence and by the seeming lack of a
ligament. From TitanosarcoUtes it differs by the lack of longitudinal tubes,
and by the inner curve probably lying on the dorsal side. The nature of
the muscle attachment is not known.

Occurrence: 5 km NNW. of San Juan y Martinez, Pinar del Rio
Province, Cuba (loc. H 774, W60) occurs a curious fossil, which deserves
some attention. Another specimen (W 132) of the same kind is also included
in our collections, but unluckily the locality label has been lost. Quite
possibly it hails from the same spot.

Description: The fossils have 6 to 7 projecting flange-like ribs,
regulariy distributed around the circumference. The ribs may reach a

height of over 60 mm ! (W 132). The ribs of W 60 have been eroded. W60
is slightly curved, with an area of stretched canals, near the outer curve,
which can be taken to be a myophorous area. In view of the position of
the muscle area's of Titanosarcolites this probably is the posterior muscle
area mp. The shell in places is strongly recrystallized in both samples. It
is possible, that in these patches polygonal thin-walled canals existed. The
canals that are still present have an average diameter of 1 mm to a wall-
thickness o£± 0,1 mm. So that they are thick-walled. The transverse tabulae
of the canals are irregularly spaced, their smallest distance being a litde
greater than the canal's diameter. No marginal row of oval canals present,
but near the outer border of the shell an entirely different kind of specialized
canals occurs, chiefly in the nbs. The canals, that are much stretched here
parallel to the outer surface, are often constricted in the middle by the
appearance of a ridge (Pl. 2, f 9). In section such a ridge presents itself
in the shape of a denticule, not unlike those of a Hippurite pore. The
ridge is mostly situated on that side of the canal, which is farthest away
from the shell' surface, pointing towards it. In places there is a ridge on
the other side as well, the two ridges facing each other or alternating.

Association: with Camerina dickersoni (W 60 and W 132) and Orhi-
toides apiculata (W 132) ; so the Maestrichtian age of the fossils is proved.

Observations: The fossils differ from Antillocaprina by the presence
of the enormous ribs and from both that genus and Titanosarcolites by the
entire absence of the normal marginal canals, and the presence of the differ-
ently specialized canals. Other differences of course may exist in the dentition.
This is a more specialized species, more of a sideline than the former.

1924 (Titanosarcolites) Trechmann, C. T. — Geol. Mag., 61, p. 397.
1926 (Diatretus) Douvillé, H. — C. R. S. g. F., p. 71.
Genotype: Caprintda gigantea Whitfield.
Distribution: Jamaica, Cuba, St. Croix?, Chiapas? i).
It is proved by Douvillé's words on p. 132 of the B. S. g. F. of 1926,
that the name Diatretus is a synonym. It cannot be used again.

Titanosarcolites giganteus (Whitfield) Trechmann. (Pl. 2, ff. 1—7, 10,
llab; 3, f. 3; 9, f 1).

1897nbsp;(Caprinulagigantea) Whitfield, R. P. — Bull. Am. Mus. Nat. Hist., 9,
pp. 194—196; Pl. 18; 19, ff 1, 2; 20; 21; 22, ff 1—3.

1898nbsp;(Caprinola g.) Douvillé, H. — Rev. crit. Paléoz., 2, 3, pp. 123, 124.
(1923 (Caprinulag. ?) Stanton, T. W. in Vaughan, T. W. — Journ. Washing-
ton Ac. Sc., 13, No. 14, p. 305.

m) Muellerried 1934, p. 81: .......and finally, pachyodonts of somewhat uncertain systematical

position, but belonging to the genus Diatretus Douvillé, i. e. several subgenera and species, from Jamaica,
Cuba and Chiapas, amongst them Titanosarcolites gigantea (Whitfield)quot; (author's translation).

1924 (Titanosarcolites giganteus) Trechmann, C. T. — Geol Mag 61
pp. 397—400; textf. 1 ; PL 23, ff. 1, 2.nbsp;'

1926 (Titanosarcolites gigantea) SAnchez y Roig, M. — Mem. Soc Felipe
Poey, 7, pp. 93—95; PL 7.

1926 (T. giganteus) Douvillé, H. — B. S. g. F., (4) 26, pp. 131—133; PL 8,
f. 5.

1934 (Diatretus, Titanosarcolites gigantea) Muellerried, F. K. G. — An.
Inst. Biol. Mexico, 5, 1, p. 81 i).

textf 3 (12). (with the exception of H 627, cf p. 84).
(1937 (T. g.) Vermunt, L. W. J. — Journ. Pal. (in press).

I have at my disposal 36 specimens of this form. One from Catadupa,
Jamaica, from the Basel Museum, the others from diverse Cuban localities
grouped around the following villages: Pinar del Rio Province: Rio Feo,
San Juan y Martinez, Tranca, (San Diego de los Banos); Southern Santa
Clara: Abra de Castellon, Fomento, Constancia; Camaguey Province:
Najassa, Guaicanamar, Tio Pedro, Ingenio Grande. The specimen described
by Sanchez and Douvillé came from the locality Arroyo Hondo, also
situated in Camaguey province.

The preservation of the fossils is rather like that of Trechmann's ma-
terial, and shows their great brittleness, even before fossilization !

Of the internal features hardly ever a trace could be found. In most
specimens, therefore, the orientation is entirely uncertain, and we do not
even know for certain, whether they are left or right valves. Valuable
evidence was yielded by samples Ca 70, Ca 81 and (W 64). As no tubes
could be found in the latter, we cannot be sure, whether it belongs to the
genus. Therefore it is put in brackets, when mentioned. Further evidence
was furnished by Whitfield's pi. 21 (copied on PL 2, f 6) ; Douvillé's
PL 8 fig. 5 (1926) (copied on PL 3, £ 3) and by Trechmann's description.
None of my specimens yielded conclusive evidence on all important points.
As the material may be heterogeneous, i. e. belong to different species, a
feature found in one specimen need not hold for all. But I have no means
to judge this point, so I will treat all as one species. For the sake of later
investigators, to every feature described will be added the samples that
testified on the point.

External features: Highly variable forms, attaining enormous size.
More or less arched in one plane, sometimes a little twisted in addition

(Ca 80, W 65). Recumbent, cf. Trechmann 1924, p. 387. At the convex
side there are strong flange-like ribs, with very deep grooves between
(Ca 68, Ca 70, S 67, S 65; Trechmann, p. 398). The grooves sometimes
almost occluded by a gradual thickening of the ribs towards the periphery
(Ca 68, S 65) (Pl. 2, f 7). In Ca 70 the position of this region, relative to the
area's of muscle attachment, proves it to be the siphonal region, as might
have been expected (PI. 2, f. 5). In the same specimen the inner curve appears
to be on the anterior side. The same holds for the small specimen Ca 81.
In other cases, however, the inner curve is found much nearer to the dorsal
side, but never so dorsally as in Antillocaprina (Trechmann, p. 400 ; Whit-
field, PL 21 ; S 69). In short, the inner curve is always shifted toward the
anterior side to a lesser or greater extent. Now in the large arched samples,
the plane of curvature must be and indeed is parallel to the horizontal plane
(the longest axis of the section) as otherwise the fossil would lose its equili-
brium. But in the small sample Ca 81 there is a distinct angle between the
plane of curvature and the flattened anterior face. So, during growth, this
fossil would have to shift its plane of curvature, after which it would develop
into a form of the type of Whitfield's PL 21 (cf PL 2, f 6). If not, it
would after a time, topple over upon its ventral side. In that case it
would afterwards expand along this plane and develop into a form much
like Ca 70 (cf PL 2, f 5).

It may be remarked, that not only the left valves (cf Trechmann
1924, p. 398), but also some of the large right valves (S 69; Whit-
field, PL 21 ) have a smooth anterio-ventral side. This point will be dealt
with later in the discussion on the origin of the tubes.

Internal features: Ligament found in 3 instances ^ouvillé, PL 8,
f. 5; Ca 81 ; (W 64). If we remember, that in Antillocaprina annulata the li-
gament could not or scarcely be detected in more than half of the right
valves, and in none of the left valves, we may assume, that it is always present
in principle, but hardly ever visible in the present genus. It is shaped and
situated like that of Antillocaprina. Its material has not been found.

Tooth alveoles found in several instances (Whitfield, PL 21 !;
Douvillé, PL 8, f 5; W 57; S 69; Catadupa). The posterior tooth itself
was found in Ca 81 (PL 2, f 3). Piv' much flattened against the body
cavity by the ligament (PL 2, ff. 4,6; 3, f 3). An' farther away from it (Whit-
field, PL 21). In the Catadupa sample the Piv' alveole is separated from
the visceral chamber by a thin lamina of ± 0,5 mm. For the distance between
An' and the body cavity see the table of measures. The distance between
An' and Piv' rather great. The general arrangement of the cardinal
elements is much as in Antillocaprina. The alveoles are traversed by concave
tabulae (cf Whitfield p. 195: „ . . two smaller cavities with funnel-shaped
septa arranged at variable distances of a fourth of an inch or less, ..quot; (0,6 mm).

Muscle area's found in 5 instances {ma in Whitfield's PL 21 ; ma and
mp in Ca 70 and (W 64); mp in Ca 81 and S 65a). The posterior muscle
appears to have been attached to a raised myophorous apophysis in the

left valve 2) which fits into an alveole of the right valve (Ca 81, S 65a)
(PI. 2, S. 3, 4). This alveole is separated from the body cavity by a thin
lamina about 1 mm thick (S65a). The great importance of this feature will
be discussed on pp. 94—105.

The anterior muscle attachment was apparendy more superficial 2), with
the impression of the left valve obliquely raised above the commissural
plane, the greatest elevation on the inner edge, as in Hippurites.

The body-cavity is very small, its section subcircular to oval, rather
irregular in outline with a distinct bulge of the wall at the mp area, espec-
ially in the left valve (Ca 81 : PI. 2, f. 1). The tabulae are frequently affixed
to one another (PI. 2, f. 6). Occasionnaly they have a lacunar structure, that
in horizontal section looks just like the canal-structure, to such an extent,
that the margin of the inner cavity may be difficult to locate.

Structure: No outer shell-layer. The inner shell-layer sometimes with
radially stretched marginal canals, mostly on the dorso-postenor side 3)
in one case (Ca 75) surrounding what may be a half-eroded tube. They
are mostly reduced, oval-shaped in section, and not situated in a continuous
row, but often relieved by canals of the common polygonal type. In the
Catadupa sample on the other hand, there is a continuous row of well
developed, though very irregular marginal canals. The length of their lumen
may even exceed 2 mm. In the marginal canals concave tabulae occur, at
irregular distances. Sometimes there are scarcely any tabulae at all (Catadupa).
The other canals are not differentiated into different area's. They are of rather
uniform diameter of about 1 mm or a litde less. Their tabulae are concave,
irregularly spaced. On the whole the distance between the tabulae is greater,
and often much greater than the canal's diameter, but the tabulae are by
no means as scarce as in Antillocaprina crassitela. All canals thick-walled.
In the samples (W64), Ca81, Ca 70 the canals are distinctly radially
stretched in the muscle area's (PI. 9, f 1) (cf p. 72), but in most other
samples the structure has been obscured, and the muscle area's could not
be located.

The longitudinal tubes occur by preference in a belt along the anterio-
ventral side, i.e. the place of contact with the substratum! A second patch
occurs dorsad of the cardinal apparatus. Frequendy these two regions
form one continuous sweep from the Piv' Jregion down the anterio-ventral
side toward the siphonal region (cf Whitfield, PI. 21). However, the
tubes may, it seems, occur as well in all other places, but in the cardinal
apparatus.

These tubes probably originated in the way suggested by Trechmann
(p. 397): „by a repeated growing over as the shell increases in sizequot;. The
ribs thicken peripherally, getting a knobbed section; and finally the grooves

2) Trechmann p. 400 says: „On the anterior side of the living chamber the base of an apophysis for a
muscular attachment appearsquot;, but from his fig. of this (PI. 23, fig. 2) and the accompanying explanation
(p. 408) it is clear, that he refers in reality to the posterior myophore.

The observations of Lupher and Packard on Lithocalamus indicate that this is an argument in favour
of the author's (and Trechmann's) assumption, that the animal reposed upon its anterio-ventral side.

between, are entirely overgrown (Ca 77: Pl. 2, £ 11 b) There is a difference
between this T-beam like thickening of the ribs between future tubes,
and the gradual thickening of the ribs between the siphonal grooves. In
accordance with this explanation, the tubes are devoid of tabulae (observed
for instance in S 65): they are mere enclosures of the world outside into the
animal's shell When a tube has been formed the shell at once proceeds
to form new ribs, which will eventually lead to the formation of new tubes
(Pl. 2, f. 11 a). It has been observed by Whitfield (pp. 194,195) and Douvillé
(1926, p. 131), that young specimens are more strongly tibbed, whereas
the large ones are comparatively smooth. It has already been remarked
upon, on p. 87, that the large samples may even be entirely smooth on the
anterio-ventral, the tube-bearing (1) side. This smoothness, then, probably
indicates, that the animal has reached the adult stage, where the shell increases
no more in thickness and where no ribs, and consequently no tubes, are
formed any longer.

In some specimina (Catadupa, etc.) some smaller holes are found
between the tubes. They are much smaller, but larger than the canals,
and are irregular in outline. In vertical section they appear to cross the
structure in all directions, so that it is evident, that they are bore-holes
of some mining organism. It is of interest to note, that they are entirely
contained within the canal-bearing shell-structure, sometimes cutting
through a canal, but never through a tube, which shows once again, that
the tubes are mere enclosures of the outer world

It might be thought, that the tubes are formed by the enveloping of
some symbiotic organism. This possibility cannot be excluded, but hardly
seems probable to me, because of their preference for the anterio-ventral
to dorsal belt, and furthermore because they are parallel to the canals.

Some of the tubes are irregularly shaped. The greater part of these
have a constriction down the middle, caused by the appearance of a longi-
tudinal ridge (cf Pl. 2, f 10 c-f), showing that either two grooves may be
overgrown together as one, or, that a tube may be subdivided into two
by the formation of the longitudinal ridge. This may be tested by looking,
whether such a ridge ever occurs on the external side of a tube, in which
case the second explanation would be the only feasible one. The irregular
tube on Whitfield's Pl. 21 (cf Pl. 2, f 10 c) with its tangential position
carries no weight, as ribs may shoot off in all kinds of directions, I am
indeed inclined to favour the first explanation, and most of the available

In the author's opinion Thiadens's fig. 3 (12) (specimen S. 67) does not represent such a growing
over of future tubes, but an abnormally developed siphonal region.

') These tubes resemble in a way those of the outer shell-layer of RadioUtdla, but these, it seems, are
not visible on the surface near the umbo. Should this be true,- than it will take a great deal to explain them,
as then they cannot be regarded as surface grooves grown over by the ad)oining ribs

«) It is not clear whether these holes were bored during the life of the Rudist, or afterwards. There
is no sign of regeneration, but then there could not be any, as the canals arc tabulated.

could be ascertained: Camerina dickersoni {^il^), 78, 81, 82 and at loc. H689),
Orbitoides (loc. H 689), Vaughanina (Ca 84, loc. uncertain), Biradiolites lum-
hricoides (Ca 81 amp; 82), Bournonia sp. (Ca 81 amp; 82) and Bournonia n. sect. sp. 4
(loc. H 689).

( 40 anterio-post.)
(120 through alveole)
( 70 anterio-post.)
( 60 through siphonal region)
(27 through mp)

breadth of lumen 0,4 (0,3 —0,5 )
thickness radial walls 0,07 (0,05—0,09)
distance tabulae
Polygonal canals, mean

Historical : Douvillé (1898, Rev. Crit., pp. 123,124 ; 1898, B. S. g. F., (3)
26, p. 154), judging from Whitfield's description, mistook the canal-
bearing layer for the prismatic exterior shell-layer of a Radiolitid, comparing
the fossil with Ichthyosarcolites, where: „also the canals might be in the
external layerquot;. But afterwards after having received some material (1926,
B. S. g. F.), he corrected his opinion, and pointed out, that the canals belong
to the inner shell-layer. For Ichthyosarcolites this view had already been
expressed by him in 1904 (B. S. g. F., (4) 4, p. 525).

Our knowledge has been increased on several important points by
Trechmann, who recognized the impossibility of retaining this genus amongst
the Caprinidae. Under the impression, that the cardinal apparatus fitted into
the body cavity he conferred the fossil to the Radiolitidae. As has been
shown, however, there is a distinct limit between the visceral chamber
and the tooth alveoles. Only the „innermost tabulated partquot; is the body
cavity, the tooth alveoles being independently tabulated.

Douvillé in 1926 (B. S. g. F. p. 132) points out, that the genus has a
Monopleurid arrangement of the cardinal apparatus, „rappelant jusqu'à
un certain point ceux des Petalodontia de la craie inférieure du Mexiquequot;.
The structure was found to be similar to that of Coralliochama, Antillocaprina,
Ichthyosarcolites and Rousselia. Both structure and dentition point to a rela-
tionship with Rousselia.

The writer's studies have shown, that the cardinal apparatus of Titano-
sarcolites is of a different kind still: i. e. that of Trechmannella and Hippurites.
The relationship of the genus with Antillocaprina is not doubtful and it is
clear, that Titanosarcolites with its more specialized dentition and aberrant
structure must be the derived form. It developed from the other form
through the following changes : the inner curve shifted towards the anterior
side, the posterior muscle impression of the left valve became a raised
myophorous apophysis, fitting into an alveole of the right valve; at the
same time the shell started to form the curious tubes, and, at least anterio-
ventrally the marginal canals became shorter and less clear, if they did not
lose their identity entirely. Antillocaprina in its turn must have developed
from a Monopleurid ancestor, just as Rousselia in Europe, but independently
from it.

cf n 399 The living chamber is comparatively small, but that of the left valve is deep and the
innermS; p^rt of both valves is septatequot;, and again p. 400: „These teeth are fused together m the living
chambcr, but divide where they emerge.quot;

Stratigraphically, Titamsarcolites and Antillocaprina appear to have been
contemporaneous: in Logie Green, Jamaica, TitanosarcoUtes was found
below and above a niveau with Antillocaprina occidentalis. Orbitoids were
found associated with Antillocaprina at Blue Mountain Peak, Jamaica and
with TitanosarcoUtes in Camaguey Province, Cuba {Vaughanina).

Lithocalamus colonicus Lupher amp; Packard.
1930 Lupher, R. L. amp; Packard, E. L. — 1. c., pp. 208—212; textf 1 • PI 4

Age: contained in a fossiliferous boulder, which occurs in a Pleistocene
placer gravel. Presumably of „Lower Chicoquot; origin, which as far as I was
able to ascertain would probably mean Cenomanian-Turonian.

Discussion: This fossil shows many points of similarity with this
group, which at the same dme separate it from Coralliochama-. a) absence
of a true fibrous outer shell-layer; b) presence, if not throughout the peri-
phery, of a marginal row of radially stretched canals in the right valve
(rounded-rectangular to elongate-elliptical in section); c) proximity of the
two cardinal teeth of the left valve; d) absence of a ligamental groove
on the exterior.

Indeed there are but a few points of difference between this genus
and Antillocaprina-. a) The Oregon genus is extremely gregarious: it was
affixed with the endre anterior face to specimens of its kind, and the marginal
canals are developed in such parts of the periphery only, as were not in
contact with the „substratumquot; ; thus far no ligament has been found.

As observed, it is more than likely, that this form belongs to the group
at hand somewhere in the neighbourhood of Antillocaprina. I am confident
that the eventual finding of a left valve will confirm this view.

Genus Imtnanitas Palmer 1928.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 28—30.

Type species : Immanitas anahuacensis Palmer.
1928 Palmer, R. H. — loc. cit., pp. 30—32 ; PI. 1 ; 2, ff. 1—3 ; 3 ; 4, ff. 1, 2.

This curious genus has been well defined by its author, but its features
have not been correlated with those of other known genera. It has evidently
much in common with the forms described here : the denddon consisdng
of „two protuberances with an intervening depression in one valve and

two corresponding depressions and a tooth in the otherquot; ; furthermore the
existence of numerous minute polygonal canals that are tabulated near the
centre, the closely tabulated body cavity, the absence of an outer shell layer
and the absence of a septum in either valve. It is a pity that the author
has not indicated the teeth in the figures, as these are not very clear on this
point. So the reader is left to guess their position and any attempt at a
correlation, without an examination of the material itself, is doomed to
failure. The more so, as, what is called the dorsal side of the animal in the
text, is called the ventral side in the explanation of Pl. 2, f 1.

The position of the dentition „located in the shell-wall itselfquot; and the
lack of myophores might mark an evolutional stage like that of Antilloca-
prina and Rousselia.

This animal was doubtfully referred to the genus by its author. Some
further material indeed is required. I am in some doubt as to the correlation
of the features of this species with those of the former. Namely, in Palmer's
interpretation of them, the body cavity would lie close to the dorsal side,
instead of the anterior, which, though possible of course, is not probable.
Moreover, there would be scarcely any room for the dentition and muscle
impression area's between „IFquot; and the body cavity. This entire area is
occupied by a lunular mass of polygonal canals, which is reminiscent of
the area's of muscle attachment in Antillocaprina, as well in shape as in
position. The „longitudinal cavitiesquot; then would be part of the dentition,
and their peculiar structure might be explained, perhaps, as either the
structure of the tooth or teeth, or as a posthumous filling of the alveoles
or alveole, depending on whether we have a left or right valve.

To obtain a good understanding of the following, it is necessary to
repeat in short the general principles of the classification of inverse Rudists,
as set forth by Douvillé i) and Paquier 2). This classification is based upon
the insertion of the posterior muscle.

In the Monopleurids the posterior muscle is attached to a mere thickening
of the shell-wall. In the more evoluated forms the left valve develops a
myophorous lamina (Petalodontia, Radiolitinae-, Himeraelites). The muscle is
inserted upon the external face of this lamina, while in the right valve,
still attached to a thickening of the shell-wall. In the more primitive Mono-
pleurae the dentition is nearly symmetric, and symmetrically arranged with
regard to the plane of curvature. If we draw a line through the cardinal
elements, we find that it has its sharpest bend in the posterior tooth. The
posterior muscle impression is situated upon one arm of a V, while the
anterior impression and the two teeth are situated upon the other.

In Rousselia the muscle insertions are described to be : „marginaux et
portés sur la valve supérieure par deux épaississemènts du test qui s'élèvent
obliquement un peu au-dessus du plan de la commissure des valvesquot; 3).
Thus, Douvillé concludes : a Monopleurid origin of this genus is not
doubtful. The arrangement of the dentition is entirely as described above.

The posterior muscle arrangement of the Caprinids takes the shape of
an erect lamina in the right valve, separated from the outer margin by a
submarginal cavity ö;;/^, which may be partitioned or not (cf pp. 144 seq.). In
some forms with peripheral canals in the right valve, a prolongation of this
peripheral canal-row is found outside the omp cavity. Into the cavity fits
a myophorous lamina of the left valve, outside of which in most forms the
marginal canals of that valve are found. The muscle is attached to the inner
face of the lamina of the left and to the outer face of that of the right valve.
The best figures of this arrangement have been given by Parona 4) and
Paquier Inside of the myophorous lamina of the left valve a large ex-
tension of the alveole is found : the well-known accessory cavity, which
is separated from the visceral chamber by a septum«). The ligament is

1) Douvillé 1889, B. S. g. F., lt;3) 17, pp. 644—648. Cf. also:
Douvillé 1900, B. S. g. F., (3) 28, p. 210.

Doiatillé seems to have abandoned this classification in 1936, B. S. g. F (5) 5 no 335sea
i') Paquier 1905, Mém. S. g. F., 13, fasc. 4 (Mém. 29), pp. 49—53 etc ' ' 'nbsp;l'

=quot;) Douvillé 1898, B. S. g. F., (3) 26, p. 151. Also in 1904, B. S. g. F., (4)4, p.525- PI 13 f 6
«) Parona 1908, Atti R. Acc. Lincei, Roma, Mem., 7, pp. 330 331 ■ textfics 8—12 ' ' ' '

Paquier 1905, I.e., PI. 7 (15), figs. 10, 12.
«) To avoid confusion the term „accessoryquot; cavity had better be restricted to the extension of the 3'
alveole : «', which is inside the posterior myophore of the left valve. The cavides often found outside the
myophorous laminae or impressions, had better be referred to as oma and omp cavities. The use of the
term accessory cavity for the dorsal cavities in Vaccinites and Biradiolites has gained currency. There is no
danger of confusion here, so it may stay. Even so the term dorsal cavity is clearer.

internal, forming a deep groove, which seems to break through the outer
shell-layer. It passes deep into the inner shell-layer, where it widens at the
end. It lies beyond the anterior end of the posterior tooth, and so this tooth
is not much affected by this inward movement. If we place a secdon through
a Caprinid with the ligament up, the relative position of teeth and muscle
scars is not so different from that of the Monopleurae. A section like that,
however, is usually drawn with the curvature and thus with the anterior
side up, and then this fact is greatly obscured. The well-known asymmetry
of the Caprinid dentition is merely an asymmetry with regard to the curv-
ature.

A similar muscle arrangement to that of the former group exists m
Caprotina quot;') and allies, but here the omp of the right valve is never subdivided,
but simple and short and it bears resemblance to an alveole into which
fits the myophore of the left valve, which presents itself in the shape of a
tooth-like apophysis®). The posterior tooth and muscle apophysis of the
left valve are separated from the margin by one or a few primitive large
canals or cavities. In Chaperia with its operculate left valve these canals
are reduced^). The alveole 5' is a little extended into a small accessory
cavity i®). The ligament still is nearly external, and the arrangement of the
dentition is as in Monopleura.

The posterior muscle of Polyconites, although attached in the left valve,
Caprinid-like, to what must be considered the inner face of the myophorous
lamina, is in the right valve affixed to a mere thickening of the shell-wall,
Monopleura-Y\kt. This form is therefore a litde enigmatical, but on the whole
it seems safest to accept a Monopleurid origin for it, as was the opinion
of Douvillé in 1889 (but not in 1900, vide note 1, when both Horiopleura
and Poljconites were reckoned by him to the „deuxième groupequot; i. e. Gyro-

') The name Caproiina has no status in its present sense. Thcoreticdly, it is the valid name for one of the
following genera: Apricardia, Baykia, Gyropleura, Matheronia, Monopleura, Requmua, loucas,a
pleura znd Requienia only, when d'ordigny's „Quelques Considerations sur les Brachiopodes really has
priority over Mathéron's „Catalogue Méthodiquequot;), and probably for Reqmema, through page priority
(so if Mathéron has priority, one could conveniently take CaprotinaJoT a synonym ofnbsp;No a

kgle one of the species listed now as Caprotina (cf. Kutassy, 1934, Foss. Cat., 68, p^ 134-141). occurs
under that name in d'orbiony's Considérations. Without exception, they are named Caprwa. His species
oi Caprotina (ammonia, lonsdalei, trilobata, lamellosa, rugosa, navis, laevigata, arch,aaana, car,nata. subaefugt;hs-,
the two last-named only „Caprotinaquot; in the notes, but Caprinaquot; in the text), have all been Pl^ced m one
of the above-mentioned genera since. Chaperia costata is certainly not the type of p^r./zw^ Jf. Kutassy,
Cat., p. 134), for this species also is listed as Caprina. Moreover in that case Chapcna would have to be

quot;quot;i'£''ibóvc-mentioned gcneric names, may be submitted as nomina conservanda, for they are well
defined Thiris not the case^ith the present assemblage of so-called Caprot,nae %o to propose
as a nomen conservandum in its present sense, or to make a new name, would be nonsensical as there is
no pïesTnt seLe. For this reason the name is used here, but ts use is restricted for such forms as str,ata.
«) Douvillé 1886, B.S.g.F., (3) 14, p. 395; textfig 11.

'») Douvillé 1887, B. S. g.F., (3) 15, pp. 776, 777. It is not clear, whether this holds true for all forms

concgnednbsp;^^^ Caprotinae directly from Gyropleura through Horiopleura and seems

to look upon the smallness of the accessory cavity in Caprotina as a primitive feature. Paquier, 1. c, pp. 56,
58 demonstrated that an accessory cavity is well developed in Hor,opUura. In Ethra which he accepts as an
Sern^dkry stage between Horiopleura and Caprotina, it is greater süll. So he condudes that the accessory
cav t^ was afSards reduced and that its smallness in Caprotina is secondary (cf. Paquier, I.e., p. 51).

pleurid group) and of Paquier (Lc., p. 50). Horiopleura is very similar,
but differs in having the posterior muscle attachment a litde individualized,
already protruding a litde, lamina-like into the body-cavity. For this reason
it was thought to have derived from the Gjropleurinae. The difference though
seems not to be so great, as is proved by Douvillé's textfigs. 14 and 15,
p. 644, 1889, Lc. For even though they are not correct ^i), they illustrate
Douvillé's conception of the difference. The sections of true Horiopleurae
figured until now, are practically all tangential. So in order to get a good
view of a radial section, I have had a specimen of Horiopktira lamherti

Progressive development of posterior muscle
^ area in the Polyconitinae, cf. p. 104.

Fig. 1. Polyconites douvillet Di-Stef., drawn
after Di Stefano, G., 1898, Pal. It., 4, Pl. 4,
f. 5c. Oblique tangential section through the
posterior region. Posterior muscle area distinctly
inclined.

Fig. 2. Polyconites boehmi Di-Stef., drwan
after Di Stefano, G., 1. c., Pl. 2, f. 3b. Oblique
tangendal section through the posterior region.

Fig. 3. Horiopleura lamherti (Mun.-Chalm.),
from Western Ibiza. Proximo-distad secrion.
Owing to the shell's curvature, the section is a
little oblique to horizontal, near the umbo. So
the overhanging of the visceral cavity is exagge-
rated, as we merely pass out of the mp region,
near the bottom. Origin of an amp cavity, mp
bluff, not lamina-like.

Fig. 4. Horiopleura haydeni Douv., after Dou-
villé, H., 1926, Rec. Geol. Surv. India, p. 352,
f. 5. Proximo-distad section. The omp cavity more
developed. The muscle area is still bounded at
the inside by a vertical wall, i. e. a wall in the
direction of growth (cf. p. 104, note 30).

Note gradual and systematically unimportant
difference between the Polyconites and Horiopleura
mp area. The figures are slightly deceiving, because
of the first two being tangential. Di Stefano's
section, however, were cut so, that the diffe-
rence is not essential.

(Mun.-Ch.) from Western Ibiza 12) cut through in this direction. This section
is herewith figured (fig. 3). It is clear, that the posterior muscle insertion
does not bear resemblance to a real lamina, but that it is more like a bluff
thickening of the shell-wall, overhanging the umbonal parts of the visceral
chamber. On account of all this I have come to the conclusion that the
genus is closely related to Polyconites, and thus also of Monopleurid origin.

quot;) cf. Di Stefano 1899, Palaeontogr, It., 4, p. 39. The specimen docs not belong to Horiopleura, but to
Polyconites species douvillei Di Stefano 1899. The posterior muscle inserdon is as in Polyconites, a thickening
of the shell-wall, a little inclined towards the interior at first: the true muscle scar, and then steeply down-
ward.

The habitus also is much like that of Poljconites. There are of course some
differences, enough to warrant the generic separation.

In Trechmannella and in the Hippuritinae we find a peculiar type of
cardinal arrangement that may be described to the full. The posterior muscle
is attached in the left valve to a raised myophorous apophysis, which fits
tooth-like into an alveole of the right valve, as in Caprotina, This alveole
is separated from the visceral chamber by a thin wall. The muscle is

PI. 5. f 2 and PI. 6, f. 1 (Univ. Oregon Publ., Geol. Ser. 1, 3), wuh regard to the text

Fig. 5. „Hippurites requieni Math.quot;, after Douvillé, H 1893 Mem. S. g F., 3 (Mém. 6) PI 8
f. 5 (nec H. requie^ according to Kühn, O., 1932, Foss. Cat. 54, p. 63). Ligament connected ; outer shell
layer developed • posterior tooth not as narrowly linked with ligament as in Anttllocaprma ; siphonal pillars.
The anterior area is much more extended, than in Antillocaprwa.

Fig. 6. Trechmannella persica Cox, after Cox, L. R., m P'^oc. Malac. Soc., 21 1, f. 4. The myo-
cardinal lamina is only just hit at „.quot; ; its nature is better visible in Cox's textf. 3 which is a lquot;tle higher.
The lower section was chosen here, to emphasize the similarity with 7ttanosar ohtes (cf PI. 2, f. 4). Outer
shell layer developed; ligamental cavity in exactly the same position as the ligamental rudiment of

N.B. the obliqueness of the longest axis in figures 3 and 6 is caused by the shifting of the curvature.

inserted upon the inner face of this myophore in Hippurites, according to
Douvillé and the same is considered to be the z2J=gt;^mTrechmannella^'^).
The anterior muscle scar of the left valve is obliquely raised above the
plane of commissure, with the inner edge elevated the most, even to such
an extent as to thin out into a myophorous lamina (Trechmannella), which
is nearly perpendicular to the commissural plane. The muscle, then, is born
upon its external face. In Trechmannella this lamina is bounded externally
by a shallow submarginal depression. The tooth 3 of the right valve is
reduced and there is no corresponding alveole in the left valve and, a fortiori
no extension of it into an accessory cavity. The cardinal apparatus is
asymmetric with regard to the curvature, which is anteriorly directed. The
ligament is much advanced towards the interior and rudimental. But here
it lies not beyond the anterior end of the posterior tooth, or, at least, it
is closely connected with this tooth. And so the Piv was pushed towards
the interior by the ligament. As a result, the anterior tooth now lies at the
sharpest bend of the dentition line. Here it is the anterior muscle impression,
which forms one arm of the V, whilst the other is formed by the posterior
muscle lamina and the two teeth. This, as it were inverted, asymmetry is
accentuated by the shifting of the curvature towards the anterior side
(Trechmannella, Torreites) i®).

Now let us return to Antillocaprina and Titanosarcolites. It has been
seen on p. 91, that these two genera are closely related to one another,
and that Titanosarcolites with its complicated shell-structure must be consid-
ered the derived form. The more original form Antillocaprina has so much
in common with Rousselia, that it would be forced, not to accept a close
relationship between them. And so we must accept a common, i. e. a Mono-
pleurid origin for them. This is born out by the following fact: The alveole
lt;3', which, luckily is still present, is not in the least extended. The posterior
muscle insertion is not well known and cannot be brought into the argument.

The dentition is almost perfectly symmetrical. This may be explained
in the following way, if we take the primitive dentition arrangement of
Monopleura, Gjropleura and Caprotina for a starting-point. The curvature of
the left valve is still symmetrical with regard to the dentition. The ligament,
on the other hand, has advanced far towards the interior. This pushed the
posterior tooth inward, but a shifting of the curvature is needed to enable
the anterior tooth to take up the position it has in Trechmannella and the
Hippuritinae.

This final change was effected in Titanosarcolites. The curvature did
shift towards the anterior side, and the anterior tooth took up a Trechmannella-
like position. The posterior muscle insertion, which is known here, is ex-
actly as in Caprotina, Trechmannella and Hippurites.

quot;) Douvillé 1890, Mém. S. g. F., 1 (Mém. 6), p. 3.
Cox 1934, Proc. Malac. Soc., 21, pt. 1, pp. 64—66.

The position of the dentition relative to the ligament is different in some Hippuritinae, because of the
enormous development of the anterio-dorsal side {Vaccinites), and the narrowing of the posterior side.

Now the important point is, that the cardinal apparatus of Titano-
sarcolites is scarcely different at all from that of Trechmannella and Hippurites.
For these forms a Caprotinid origin is generally accepted i«), but it has
been seen that the posterior muscle attachment of Rousselia and the nature
of the 3' alveole oi Antillocaprina exclude such an origin for Titanosarcolites.
As a consequence of this a cardinal apparatus of this type may develop
independently, without any connection at all with the Caprotinids, and from
a type more primitive still, i. e. a Monopleurid type. And thus some doubt
is thrown upon the Caprotinid origin of the other two forms as well. So
we must examine the arguments, which have led to the acceptance of such
an origin. The following arguments have been or may be brought to the fore.

a)nbsp;The posterior muscle arrangement, the presence of a myophorous
lamina in the right valve, the asymmetry of the dentition with the antenor
tooth at the sharpest bend i'). All these features have been effected in
Titanosarcolites without the intermediary of a Caprotina or even a Gyropleura.

b)nbsp;The presence of canals. This is a feature that occurs in all inverse
Rudist groups (cf Chiapasella) and is, therefore, of no consequence. It
merely marks an innate tendency of the entire group.

c)nbsp;The 3' alveole is no longer developed in the forms at issue and
cannot bear witness, but the mere fact, that the two teeth and the flip are
on one line, makes it hardly possible that there can ever have been any
extension into an accessory cavity.

d)nbsp;The reduction of tooth 3 and the greater prominence of the left
valve's myophorous lamina with regard to that of the right one is). These
features exclude the Caprininae as a possible source, it is true, but give no
further clue, as they occur also in direct descendants of the Monopleurinae.
For instance : reduction of tooth 3 in all Radiolitinae, greater prominence

As a result the arguments named do not point conclusively to a Capro-
tinid origin, and the evolution of the Antillocaprininae forms an argument

striata, quadripartita) and Chaperia the ligament lies beyond the antenor
side of the posterior tooth. So, if it started to advance towards the interior,
the tooth would not be caught between the ligament and the body cavity,
but merely be drawn with it towards the interior. In Monopleura (imbricata,
michaillensis) it is situated against the anterior end of the posterior tooth.
This, then, would explain the situation in Antillocaprina, as well as that
of Titanosarcolites and Trechmannella.

S?rox^q34 t'/^P 65 compares the main bend in the margin of the hinge plate in Caprotina with
that of Trechmannella. Thi^ must not be confused with the main bend in the dentition line meant here. In
TrecLamella the two coincide. Not so in Caprotina because of the presence of an accessory cavity (cf. for

One might object to a Monopleurid origin of the Maestrichdan
Trechmannella on account of the absence so far of Monopleurae in the
Senonian strata, but such an origin will have to be accepted in any case
for the equally Maestrichtian Rousselia. Moreover this objection applies
equally to a Caprotinid origin. It merely shows how defective our know-
ledge still is.

If we go as far as this, we may as well reconsider the Caprotininae them-
selves. They descended, it has been thought, from Gyropleura, on account
of the presence of a myophorous lamina in the right valve. Now that this
argument no longer holds, it is not impossible to think, that they too
descended direcdy from the Monopleurinae. This is indeed not unlikely, for
example, for the Bohemian Caprotininae. They are much like Monopleurae
and occur in a Monopleurid associadon.

Ichthyosarcolites presents a problem because of the bad preservation of
the material, and the controversial nature of its descriptions. It is not
unlikely, that entirely different forms have been assembled under this generic
name. In any case the genus stands in great need of revision. If we take
Douvillé's description for a base it seems that the curvature is asym-
metric with regard to the dentition, and shifted towards the anterior side.
In addition the shell seems to consist entirely of inner shell-layer. The
latter fact would remove the genus from the Radiolitinae, with which it has
been united 20), and would approach it to the forms described here. The
tubular structure of this layer, and the general habitus point the same way.
The beginning of a myocardinal lamina appearing in Trechmannella 21) shows
how the cardinal apparatus of Ichthyosarcolites may have developed from
the type under discussion, independendy and without any connection
whatever with the Radiolitinae. On the other hand it may also have developed
directly from the Monopleurid type, in which case it would belong to the
first type of evolution. It would, however still be independent from the
Radiolitinae and form a branch of its own.

Immanitas is not known well enough. The absence of an outer shell-
layer, the tubular shell-structure, the dentition, which to judge from the
description was Monopleurid in nature 22)^ and the entire habitus, point
to a relationship with the Antillocaprininae.

Lithocalamus shows only one major point of difference with Antillo-
caprina, i. e. the absence of a ligament. Thus it is probably related to this
genus, but no left valve is known, and consequently we can have no cer-
tainty on the point.

Summarizing : the forms described under this heading do not constitute
a monophylum, but they represent an assemblage of forms. Indeed they
fall naturally into several groups, that cannot possibly have derived one
from the other, and it is for this reason, that they have been put into
different subfamilies. These subfamilies developed from the common
ancestral Monopleurid type, at different times, independently, but along
parallel lines of differentiation. At what exact moment these subfamilies
branched off, can, of course, be said only with reserve, as every now and
again genera are discovered to have a much greater vertical range than

The first to come was Ichthjosarcolites, which incidentally developed
much farther than any of the later subfamilies. It differentiated quite early
in Urgonian times, if we may accept the species of Paquier as a real Ichthjo-
sarcolites.

Then, at some date unknown, but before the Cenomanian, some of the
forms now included in the „Caprotininaequot; may have originated, from the
same stock, it is thought, and without the intermediary of Gjropleura. Their
cardinal evolution is a little different, because of the extension of the 3'
alveole. They present a type of evolution, which is intermediate between
that of the Caprininae and of this group. Their general nature (shell-structure I)
is different too.

After that, just before the close of the Turonian, the Hippuritinae came
into being. This group proved itself unbelievably fertile. The inner shell-
layer canals of Torreites must have developed independently just as did
those of Chiapasella in the Radiolitinae.

At the close of the Cretaceous, at three different points of the earth,
three different groups developed, nearly at the same time, viz.: Trech-
mannella in Asia, Rousselia in the Pyrenean gulf and AntiUocaprina in the

In the incipient stage, the cardinal apparatus is asymmetrical, the main
curve is dorsal, the ligament is external or nearly so, and the muscle scars
are a little raised above the plane of commissure in the left valve. In short

while atrophying at the same time. If this reduction was completed first,
before the ligament had noticeably moved, we get the dentition of a Rous-
selia. In the Antillocaprininae, Trechmannellinae and Hippuritinae, on the other
hand the ligament had already moved inward to a considerable extent.
In some Rudists the ligament may push right through the outer shell-layer,
e. g. in Sellaea In AntiUocaprina on the other hand it drags part of the
outer shell layer with it, which though becoming disconnected from the
rest of that layer continues to grow in its isolated position. In the Hippu-

quot;) cf. Di Stefano 1888, Atti R. Acc. Sc. Ictt. arti Palermo, (n. s.) 10, PI. 9, fig. 2c, and others.

ritinae, as in the Radiolitinae, the outer layer is drawn out into a longitudinal
ridge : the ligamental inflexion

Further changes take place in the cardinal apparatus. The first is another
consequence of the inward movement of the ligament and concerns the
posterior tooth. This tooth, the anterior end of which is narrowly linked
with the ligament is pushed before it, as it were, and finds itself caught
in the end, between the ligament and the living chamber. This is the situ-
ation in Antillocaprina for instance. The dentition, as a sequel of this inward
movement, has become symmetrical. In the next phase, the curvature shifts
towards the anterior side and the cardinal symmetry is lost. The tooth 3
becomes much reduced, and its alveole disappears, without ever having
been extended into an accessory cavity. At the same time the left valve
develops a raised posterior myophore, which fits tooth-like into a corres-
ponding alveole in the right valve. The anterior muscle scar of the left
valve becomes more and more elevated at the interior edge so as to increase
its obliqueness, until it stands nearly perpendicular to 'the commissural
plane. The corresponding muscle scar of the right valve undergoes no
important change. This evolutionary stage is represented by the Hippu-
ritinae and by Titanosarcolites amongst the Antillocaprininae. After that, a
myocardinal lamina starts to form, which runs centrad of the teeth. It is
formed by the myophorous laminae and by the interior part of the base
of the teeth. It conforms more or less to the inner edge of the myocardinal
plate of primitive rudists. Between the teeth and this lamina is wedged
the septum, which, in the right valve, separates the tooth alveoles from the
visceral chamber. This stage is reached by Trechmannella.

Thereupon, it is conceivable, the alveolar septum of the right valve
might become entirely reduced, just as happens in the Radiolitinae. The
alveoles would lose their identity and become mere „gouttièresquot;. The
myocardinal lamina of the left valve would then encompass the two teeth.
This final stage, then, would have all the general appearance of the dentition
ol-^ Biradiolites. So, if such a form were found, it would have to be recognized
by features, other than cardinal, for instance by structural differences (lack
of prismatic-cell structure in the outer shell-layer, etc.). This, then, is
exactly, what is the case in Ichthyosarcolites, and the hypothetical form
described above would be much like that genus indeed. The reasons which
link this genus with the group at hand have already been named (p. 100).
There are, however, some objections to this : first the canal-bearing layer
may yet appear to correspond to the outer shell layer. Its early appearance
is another difficulty. Lastly the above reasoning has not dealt with the
alveole for the posterior muscle apophysis. Douvillé 2«) has set forth

/') cf. Douvillé 1910, Mém. S. g. Fr., 18, Mém. 41, pp. 10, 11. It is clear, then, that the explanation
ot the origin of the Hippuntid pillars given by Douvillé, does not explain why the pillars arc formed
as forms with similar growth and cardinal arrangement {Trechmannella) did not develop them. But it can
certainly explain their number and position. In any case, the ligament of Antillocaprina presents a striking
parallel to that of the Hippuritinae.nbsp;^ fnbsp;b

cf. Douvillé 1936, B. S. g. F., (5) 5, textfig. 9b.
'i') e.g. Douvillé 1890, Mém. S. g. F., 1 (Mém. 6), p. 3.

several times, that in the Hippuritinae the posterior muscle was inserted
in the left valve to the inner face of the myophore, and in the right to the
lamina, which delimits the myophorous alveole. So it would be impossible,
for this lamina to become reduced, without further measure! Perhaps the
lamina is not reduced at all, and is represented by the lamina described by
Parona 27), (cf p. 55). But after all so much uncertainty is involved, that
we had better speculate no more about this genus.

Another change concerns the outer shell-layer, which, contrarily to
the evolution of Radiolitinae, shows a tendency to reduce. In the American
forms this layer has never been demonstrated beyond doubt, and I am
convinced, that in Titanosarcolites at least it did not exist, as I have never
found any trace of it in the tubes. In Antillocaprina it was never found
either (cf p. 71), although several of the accompanying Mitrocaprinae still
retained patches of it. In the Hippuritinae and Trechmannella it is well
developed ; in Rousselia it is present, but thin.

In the inner shell-layer of most of the described forms a multitude of
polygonal to rounded canals occur. In the American forms they traverse
both valves, invading the entire cardinal apparatus. In the Eurasian Trech-
mannella and Rousselia, they occur only in the right valve. Those of the
first genus are at variance by their great size. Even in the Hippuritinae
they appear towards the close of the period, in the Cuban Torreites. Their
appearance here is obviously independent from that in the other groups.
They occur in this genus in the left valve only.

Finally, the animals increase their size, reaching enormous dimensions
(Ichthjosarcolites, Parastroma, Titanosarcolites). This is a characteristic shared

The Monopleurid or first type of evolution differs mainly in the
following respects : The final stage of cardinal evolution — teeth and
myophorous laminae fused into one myocardinal lamina, which fits into
the right valve's body cavity — is reached, without a posterior myophorous
cavity ever having been formed in the right valve. The posterior muscle
is always attached to the outer face of the left valve's lamina. The outer
shell layer is not reduced. On the contrary in the Radiolitinae it increases
enormously in thickness, developing the peculiar and wellknown prisma-
cell structure. For the rest it is much like the evolution of the second type.
In the Radiolitinae the ligament also moves more or less inward, and in
accordance with this, the dentition becomes symmetric. Eventually in
BiradioUtes, Boumonia and especially in Chiapasella, what amounts to the
inner curve is shifted towards the anterior side, but the emancipated
dentition remains symmetrical. The ligament has disappeared in these genera.

The Caprinid or third type of evolution differs by the development
of tooth 3, which may reach a considerable size. A myophorous lamina
and cavity are well developed in the right valve. The cavity is not alveolar.

and the corresponding myophorous lamina of the left valve is not tooth-
like. The 3' alveole is extended into an accessory cavity n'. The Caprininae
descended from the Gjropleurinae according to Douvillé ^s).

The Plagioptychinae (pp. 153-155) form a parallel branch to the Caprininae.
They too developed from the Gyropleurinae, but the true Caprinid type
with erect muscle lamina in the right valve, was only imperfectly reached
in Mitrocaprina.

There are two or three branches that descend directly from the Mono-
pleurinae, but stray away into the direction of the third type of evolution.

Himeraelites, the simplest, is still essentially of a Monopleurid type as
is proved by the Monopleurid nature of its muscle insertion, however, its
curvature is shifted towards the anterior side and the 3' alveole became
greatly extended. As a result the dental arrangement is exactly as in the
Caprininae.^ Should ever a Himeraelites develop canals, as well it might, then
the resulting animal would almost certainly be taken for a Caprinid. In
other words, all forms until now described as Caprinids will have to be
carefully checked as to their muscle attachment.

^ In the Polyconitinae a cavity develops under the left valve's muscle scar,
which becomes a lamina in this way, bearing the muscle upon its lower
face. This lamina becomes more and more erect, and the muscle insertion
is swung back towards the interior. Corresponding with this, the muscle
scar of the right valve, at first inclined towards the interior upon a thickening
of the shell-wall (Polyconites), becomes parallel to the commissure (Horio-
pleura almerae) 29), until it is turned upwards, almost lamina-like, in H.
haydeni^^). The alveole 3' at the same time becomes extended.

The diagram of p. 105 illustrates the views expressed above, and gives
the distribution of the phyla over the different types of evolution.

The immediate result of this kind of grouping is, that practically all
canal-bearing genera younger than the Turonian have been removed from
the Caprininae. This subfamily seems to have reclined in the Turonian ^i).
It consists of the following genera: Pachytraga-, Praecaprina \ Caprina,
Schiosia, Orthoptychus, Sphaerucaprina ; Offneria, Caprinula ; Sabinia ; Amphi-

Douvillé, H., B. S. g. F., (3) 17, p. 647 (through the intermediary of Horiopkura).

A true lamina, parallel to the commissure, by the way, can only come into being in an exogyroid
right valve (as in Gyropleura and Plagioptychus). Otherwise it could not follow the growth of the animal.
In a conical right valve, unless we assume resorption during growth, it must either be erect, or not be a
true lamina at all.

The Schiosi and the related Sicilian Caprinid fauna's were formerly reckoned to the Cenomanian
(cf. for instance Douvillé, H., 1898, B. S. g. F., (3) 26, p. 150). In later years, however, they have been put
into the Lower Turonian (cf. for instance Douvillé, Paquier amp; Toucas in Haug, E., 1910, Traité de Géol
2 2, p 1169; Dainelli, G., 1921, La struttura delle Prealpi Friulane, p. 14). In any case, the genus
Caprinula^ho seems to occur in the Lower Turonian. From the Upper Turonian and from the Senonian
only doubtful cases are mentioned, if for the moment we leave aside the genus Sabinia. The American
forms that genus seem to occur in the Middle Cretaceous. As will be seen (pp. 145. 150), they are
of a different type, than the European Sabiniae. The latter are described from the Maestrichtian (the
Maestrichtian Schiosia bilinguis, by the way, which is certainly not a Schiosia, also may be a Sabinia)
This, now affords a curious problem. It will be discussed on pp. 150, 151.

tricoelus \ Planocaprina, Coalcomana, Caprinuloidea. Ethra may be a direct
ancestor of this group, and Sellaea seems to have descended from Ethra^).
They cannot be included amongst the true Caprinids because of the primitive
nature of their ligament and posterior muscle attachment.

quot;) It does not seem likely to me, that Sellaea descended frorn Pac^traga (cf. Paquier, 1905, Mém.
S. g. F., 13, fasc. 4 (Mém. 29), p. 69), for Pachytraga has the Caprinid features already fully developed.

Key for the Determination of the Genera of
the Second Type of Evolution.
(Excepting the Hippuritinae).

1nbsp;(2) Teeth of the left valve with their lower ends not fitting into alveoles

in the shell-wall of the right valve, fused with the myophores into
one lamina, which fits into the body-cavity of the right valve; as
in Biradiolites. Rounded canals in both valves, not tabulated. Concave
side not dorsal. No outer shell-layer known.
Urgonian-Cenomanian. Old-world tethys.

slightly, obliquely raised above the plane of the commissure. Ant-
erior tooth geniculated, large, nearer to the visceral chamber than
the posterior. No ligament found. Concave side dorsal? Outer
shell-layer thin.

valve attached to myophorous laminae, the posterior myophore
fitting into an alveole in the shell-wall of the right valve. The
myophores connected with one another and with the base of
the teeth by a thin lamina, which runs centrad of the teeth.
A ligamental cavity present, not connected with exterior, entirely
contained within the inner shell layer. Posterior tooth much nearer
to the body cavity than in Rousselia. Concave side of left valve
near the anterior tooth, in the right valve at the siphonal region.
Outer shell-layer well developed.

At about the boundary between Campanian and Maestrichtian.
Persia, Eastern Arabia.nbsp;' Trechmannellinae.

contained within the inner shell layer, with a characteristic comma-
shaped section, consisting of fibrous material; quite often, especially
in left valves not to be found. Posterior tooth not farther removed
from visceral chamber than anterior tooth.

13 (14) Marginal canals pyriform, radially stretched. Anterior and Pposterior
muscle impressions of left valve slightly, obliquely raised above
the plane of the commissure. Concave side dorsal, the cardinal
apparatus mostly symmetrically arranged with regard to the plane
of curvature.

Antillocaprina. Trechm. 1924.
14(13) Marginal canals reduced, egg-shaped in secdon. Ill-known genus
with rather sharp ribs.

stretched parallel to the circumference, these may be constricted
down the middle by one or more longitudinal ridges, mostly on
the inner side. Enormous flange-like ribs.
Maestrichdan. Cuba.nbsp;Ant. .aff. gen. B.

10 (9) Shell pervaded by longitudinal tubes. Posterior muscle inserted in
the left valve on a disdnct myophore; which fits into an alveole
in the shell-wall of the right valve. Anterior muscle impression of
left valve also raised into a ridge, bearing the muscle inserdon upon
its outer surface. Posterior tooth nearer to the body cavity, than
the anterior. Concave side more or less towards the anterior side.
Marginal canals sometimes present, mainly dorso-posteriorly, well-
developed or reduced.

Titanosarcolites. Trechm. 1924.
8 (7) No ligament found as yet. Genera of doubtful position.

15nbsp;(16) Gregarious forms, largely affixed to others of their kind or to other

objects. Marginal canals developed on those parts, that are not in
contact with the substratum.

A classification of the Hippuritinae has been given by me in a former
paper i). This classification, as was expected, was met with criticism 2). It
contains indeed an important error: the genus Pironaea has no accessory
cavity. Kuhn says, moreover, that it is not always present in Vaccinites
either. It is to be regretted, that no instance of this is cited by him. In any
case, this feature will have to be struck out in the key There are some
other corrections to be made. First the pores of Parastroma are not dentic-
ulate, but distinctly reticulate (cf PI. 10, f. 5), but the trabecules disappear
with the slightest erosion and then the pores become denticulate. In one
or two places only could their true nature be observed. Extrapolating we
may assume, that the pores-of Praeharrettia and Barrettia are also reticulate.
Secondly, although Praeharrettia cannot be sharply delimited from Barrettia,
it had better be revived after all: some samples are so similar to Pironaea,
that the difference with Barrettia becomes greater in comparison. And then,
after all, it is equally impossible to delimit Pironaea from Vaccinites. Then
a species of Torreites has been discovered (cf. p. 129), which lacks the short
infoldings of the species sanche^i. Lastly, Toucas's distinction between
the Hippurites and Vaccinites with polygonal pores can be better worded.
The forms counted by him as Hippurites have the ligament always rounded,
whereas it is truncate in those, which he regards as Vaccinites. This classi-
fication does not seem natural, it must be confessed, but it has the advantage
of not being based upon an unproved supposition. Taking everything into
account, the table becomes :

1. Pores linear, punctiform to rounded or polygonal (sometimes even
with a few denticulations). If the pores are polygonal, then the ligament
is always rounded. L short, very rarely a little larger.

1) Mac Gillavry, H. J., 1935, Proc. K. Ak. Wet. Amsterdam, 38, 5, pp. 560—565.
») Kühn, O., 1936, Pal. Zentr.bl., 8, no. 1, p. 47.

The other criticisms may be briefly passed in review, a) Hippurites and Vaccinites cannot be
considered as distinct genera. So either they are synonymous, or only subgenera. In the first case
the name Vaccinites would have to be dropped, which cannot be the reviewer's intention. So then
they must be considered as subgenera, and then the objection is trivial. Most Hippuritine genera
may be considered as subgenera. An almost continuous row of transitions has been found between
Vaccinites and Pironaea, and between Praeharrettia, Barrettia and Parastroma. b) ,,Dass die Abtrennung
aller Hippuritellen noch nicht vorgenommen wurde, kann kein Grund gegen die Existenz der Unter-
gattung seinquot;. Nor was it used as such, and the remark is based upon a misunderstanding. The point
was, that if all forms with polygonal pores have been revised, then will be the time to judge, whether
Hippuritella constitutes a natural group. Before this has been done, the use of the name Hippuritella in a
key can only result in confusion. I have no further inclination to enter the arena on the Hippuritella-a^t%\\on.

a.nbsp;pillars rudimental or orimental. L likewise. Pores linear, some-
times rounded.nbsp;Arnaudia.

II. Pores denticulate, reticulate, subreticulate or polygonal, in that case
r: // lt; 1 /4 ; a lt; 50°, and L truncate. L long, very seldom shorter.
L sometimes irrecognizable. In that case the pores are reticulate (when
eroded: denticulate, rectangular) and S and E are extraordinarily ped-
unculate.

C.nbsp;L always recognizable. r'.ult; 1/4; alt;50°. Very seldom these values
exceed these limits. In that case the pores are distinctly denticulate
or reticulate and the inner shell layer of the right valve does not
take part in the formation of the commissure, nor does it form a
sort of ledge near the border of the valve.

c.nbsp;If in the right valve open infoldings exist, these are more of
the nature of undulations of the outer shell layer. Sometimes
only undulations of the inner border of the outer shell layer
exist. In most cases no undulations at all.

d.nbsp;several infoldings of outer shell layer towards the interior, in
the right valve. These infoldings vary between such as are long
and thin, sometimes almost moniliform, and such as are short
and thickened, triangular, some of which may be open exteriorly,
but not necessarily so. Pores denticulate.

D.nbsp;L often only recognizable by analogy with its position in Prae-
barrettia, sometimes entirely effaced, r :«gt; 1/4; a gt; 55° (N.B. more
than one specimen should be examined!). S and E extraordinarily
pedunculate. The inner shell layer of the right valve enormously
developed, forming a sort of ledge near the border of the valve.
Pores reticulate (when eroded : denticulate, rectangular).

e.nbsp;L recognizable. The ledge of the inner shell layer does not take
part in the formation of the commissure : there is a little distance
between this ledge and the left valve. Several infoldings present.

t) In the neighbourhood of the genus Hippurites belongs Milovanovii's new genus Yvania. This
genus has but two canals in the left valve, the position of which with regard to the animal's orientation
is not given Few normal pores. Limbal pores enormously developed, and, if in the neighbourhood of
a canal, parallel to it, so that they cannot change into normal pores during growth, as is the case with
ordinary Hippurites.

These infoldings, L and the stems of i' and E not dissolved
into „moniliform raysquot;. Praebarrettia.
ƒ. L not recognizable (but by analogy with its position in Prae-
barrettia). The ledge of the inner shell layer takes part in the
formation of the commissure.

a. Many infoldings present. These infoldings, L and the stems
of S and E dissolved into „moniliform raysquot;.

Infoldings, L and the stems of S and E entirely effaced (only
rudiments of the rays are traceable near the outer shell layer
in P. guitarti).nbsp;Parastroma.

III. No pores. L extraordinarily elongate, longer than the shell radius.
Umbo of left valve displaced towards the anterior side, excentrical.
Inner shell layer of left valve with numerous rounded, not tabulated,
longitudinal canals.nbsp;Torreites.

Subsidiary, in case it should be proved, that the forms with polygonal pores
form a natural group :

b.nbsp;pillars distinct.nbsp;Hippurites (s. str.).
II. Pores polygonal. Hippuritella.

As the pores of Tetracionites are not known, it cannot be fitted into
this table.

Hippurites muellerriedi (Vermunt) (in litt.), (p. 123, f 2; Pl. 5, £ 6).
1924 (Hippurites (Orbignya) sp.) Trechmann, C. T. — Geol. Mag., 61,

pp. 396, 397 ; Pl. 23, f 5.
1930 (Hippurites (Hippuritella, Orbignya) cf. incisus) Muelleried, F. K. G.

— An. Inst. Biol. Mexico, 1, 2, pp. 165—168 ; textff. 1, 2.
(1933 (Hippurites (Hippuritella) cf. incisus) Muellerried, F. K. G. — Geol.

Rundschau, 23a, Salomon-Calvi Festschrift, p. 269.
1937 (Orbignya miillerriedi) Vermunt, L. W. J. — Journ. Pal. (in press).

For the invalidity of this name vide Teichert, C. amp; Miller, A. K., 1936, Am. Joum. Sc., (5) 31,
no. 185, pp. 352—362. The lawful name is Orthoceras Bruguière 1789. Hippurites must be considered, most
emphatically, as a nomen conservandum. For the invalidity of the name Orbignya vide Douvillé H. 1886
B. S. g. F., (3) 14, p. 401, note ; idem, 1904, Rev. crit. Paléoz., 8, p. 180; idem, 1906, Rev. crit. Paléoz. lo'
p. 52; Mac Gillavry, H. J., 1935, Proc. K. Ak. Wet. Amsterdam, 38, 5, p. 564.

To Vermunt's description a few remarks about the structure may be
added. One of the striking features, mentioned by Muellerried, is the
structure of the outer shell layer (p. 123, f 2). The Cuban specimens show
just the same peculiarities, which were studied in horizontal, tangential and
radial section. At first sight, the structure would seem to be essentially the
same as that of a Radiolitid outer shell layer, but after a closer inspection it
appears, that there are no prismatic cells. The horizontal and tangential
sections show its derivation from the common compact Hippuritine structure
(cf Milovanovic, B., 1933, Mém. Serv. Géol. R. Yougoslavie, 2, textfig. 64,
and the same, 1934, Ann. Géol. Pénins. Balk., 12, 1, textfig. 20). The
compact structure is only preserved in the anticlinal folds of the funnel-
plate-like lamellae, whereas in the synclinal parts, the growth took place
intermittently. Although the principle of this „Schalenauflockerungquot; is the
same as in the Radiolitinae, the result, although very similar, is essentially
different. There is a system of „funnel-platesquot;, which is undulated, but
instead of prisma-cell walls there are only more or less radially directed
walls, which start from the circumference towards the interior. Some of
them reach the inner edge of the outer shell-layer, others not. The fig. 2
on p. 123 demonstrates some of the irregularities, which sometimes are
encountered in the radial walls. As already stated, these walls correspond
to the upfoldings of the „funnel-platesquot;. They should not be confused
with the infoldings of a Barrettia, as the described structure belongs entirely
to the outer shell layer, whereas the infoldings of Barrettia are parts of the
outer shell layer, which pass into the inner shell-layer.

A similar structure may exist in Hipp, cornucopiae, cf Douvillé, H.,
1910, Mém. S. g. F., 18, Mém. 41, Pl. 7, f 3, and in „H. Lapeirouseiquot;
(= nabresinensis, according to Kühn, O., Foss. Cat., 54, p. 57), cf Parona,
C. F., 1900, Mem. R. Ac. Sc. Torino, (2) 50, Pl. 1, f 2.

The species has been found to exist in Cuba not only at the type
locality (L 818, 7 km NW. of Pinar del Rio city), but also at locality H 774,
5 km NNW. of San Juan y Martinez, Pinar del Rio Province. A typical
Barrettia-^Xi2A.2. fauna occurs at this locality, so that the species belongs to
the Maestrichtian. One specimen found at this locality and affixed to a
Chiapasella pauciplicata, has the dentition preserved, which is herewith figured
(PI. 5, f 6). It is at variance, though, because of the abnormal shape of
the ligament, and so it cannot be proved, that it belongs to this species.
This, however, is extremely probable.

Vaccinites inaequicostatus macgillavrji (Palmer) (PI. 4, ff. 1—8 ; 10, f 2).
1933 (Vaccinites macgillavry) Palmer, R. H. — Revista de Agric., 14, nos. 15,

16, pp. 97, 98 ; PL 4, f 1 ; 5, ff. 3, 4.
nec 1937 (V. macgillavrji) Vermunt, L. W. J. — Journ. Pal. (m press).

For the Vaccinites sp. of Vermunt, I.e., vide p. 118 : Vaccinites cf.
inaequicostatus macgillavryi.

Occurrence: Loma Yucatan, Camaguey Province, Cuba (type loc-
ality) ; Near Bramales, Pinar del Rio Prov., Cuba (Vacc. cf. i. macg., see
below).

Material: 22 specimina from the type locality collected by Vermunt
and M. G. Rutten (loc. V 529). The material is rather good, but more or
less worn. So the exact nature of the pores could not be found by direct
observation. Ornamentation well preserved. Several bivalve specimina, but
the left valve mostly worn down to the canals.

The samples are very uniform externally, and I have no doubt, but
that they belong to one species. Internally the forms show enormous vari-
ation. All the fundamental features used for the specific classification of
Hippurites seem to fail us here. A similar variation has been observed in
the typical form by Douvillé and De Alessandri f).

Exterior: small to large, elongately conical to cylindrical, sometimes
rapidly tapering. Left valve mostly elevated as a low cone, sometimes a
little flatter. The two „osculesquot; at a distance from the margin. Right valve
covered with strong, uniform ribs of triangular section, similar to those
of V. hoehmi. No secondary riblets I Distance from rib to rib 2—5 mm.
The ribs remain of the same strength during growth and do not dwindle
with age like those of V. oppeli do. L, S and E scarcely or not indicated
by deeper grooves upon the surface. Deeper grooves may occur also else-
where. The commissural line is undulated, a downfold conforming to a
rib (c£ PI. 10, f. 2). The section is round, irregular or oval. In the latter case
the longest axis runs proximo-distad, as in Munster's type specimen of
the typical form.

Pores: Some encrusted left valves were cut through radially. In this
way it could be established, that at least the limbal and adjacent pores are
complex, meaning, that the pores are subreticulate 5).

Internal features: The outer shell-layer („capa mediaquot; of Palmer)
is thick as in the Alpine forms, but not as thick as in the subsp. oppeli. Its
inner margin is distinctly undulated. In this respect it is similar to all the
inaequicostati from Sirone (Lombard). In all other European samples figured,
this undulation is absent or much less distinct. Some samples of oppeli also
present this undulation (De Alessandri, PI. 15, f 3). In others it is absent
(Douvillé, PI. 31, i. la).

The ligamental inflection is long and lamellar. In 19 cases out of 21 it
is slightly curved at the end, towards the anterior side. In this respect it
is similar to some samples from Sirone (de Alessandri, PI. 14, f. 5; 16, f. 5)
and to those described by Milovanovic ®) from Leposaviei (Stara Raska).

It is important to note, that by this simple means the forms with subredculate pores can be distingui-
shed.

®) p.-195: „In the lower part it is somewhat curved away from the first pillar. ... It differs furthermore
from Douvillé's specimina in being curved (the ligamental crest of all three specimens figured by Dou-

SECOND type of evolution : trechmannellid type ; continuation 1 1 3
Plate 4. Vaccinites inaequicostatus macgillavrji (Palmer).

Respectively Numeros Ca97. 99. 102. 108, 109. 110. 104. 112. Showing the great vambihty of this
form in eve riespect. In figure G the anterior muscle area of the right and left valve both and par of
Se left val7e wkh pores fs shown. X 0.8. The £'s curvature of Ca 102 is more distinct m rcahty.

In Palmer's cotype (Pl. 5, f. 4) this curvature is well marked In Cal 05 it
is straight in Cal 07 slightly curved towards the posterior side. It is dis-
tinctly rounded at the top in most samples. In others it is somewhat rugged

viLLi - Pl 30 ff 3—5 - is straight and devoid of any curvature whatever).. . . Meanwhile the ligamental
c est in one of de Alessandri's samples from Sirone, is a little curved in the same direction, and in us general
s£pe it is Sly like that from Wosavilt;5i.quot; ( same directionquot; literally: opposite direction, meanmg
opposite to the first pillar), (author's translation).

at the end. In other cases again, I got the impression, that it was disdncdv
truncate! (cf. Douvillé, p. 201 ; PI. 30, f 4).

The first pillar, J', is almost of the same length as the second, in contrast
with all related European forms, where it is distinctly shorter
i. oppeli, styriaeus, tarcentinus, etc./ Only in the sample figured by Toucas
(textfig. 172: Gösau) it is nearly of the same length as E, but this is a most
exceptional specimen, with very short E. It is short or long, but slightly
pinched at the base, or distincdy pinched, somedmes stalked as in the
form oppeli. The tangendal diameter of the head, divided by that of the
stem has its minimum in Ca98 : 1.3, its maximum in Cal 09 : 15 «). The
stalk of the latter has a length of more than 3 mm.

The second pillar, E, of all specimens is slightly or disdnctly curved
towards the anterior side, but not to the same degree as that of V. gaudryi,
taburni, atheniensis and of Pironaea poly sty la milovanovici. Only in Cal 11 it
is nearly straight. In Palmer's cotype it seems to be straight too. It is
generally more pinched than the The proportion head divided by stem
is minimum in Ca99 : 1, 5, maximum in Cal 09 : 32. The length of the stem
in the latter is more than 4 mm. The head of this pillar is more oblong
than that of the first

The angle between An—Piv and L is greater than in all European
samples, but there is no leapwise difference. There is a slight ovedap of
the two ranges of variation : European forms : 15°—35° (resp. Douvillé,
PI. 33, f. 3, Sirone and PI. 30, f. 4, Oberberg) ; Loma Yucatan forms :
25°—50° (resp. Cal04 and CalOl, 103). The posterior tooth lies alongside
the ligament's top. In Ca97, 104 the Z. is a little surpassed by it, in Cal 12,
115 distinctly. The angle An—Piv\jPiv—mp is most variable, ranging
from 165°—215° (resp. Cal 09 and Ca99). The jtip is triangular in section
in most cases, and thus truncate towards the margin, sometimes broadly
triangular. It may even be emarginate, sometimes it is more rounded.
In other cases it is longish, oval, emarginate or not. In a higher section,
then, it often becomes more distinctly emarginate or triangular lo). As is the
case in the specimina of Douvillé (PI. 30, f 3, Gösau; PI. 30, f 4, Ober-
berg; PI. 33, f 3, Sirone) and of De Alessandri (PI. 16, f 5, Sirone) it does
not surpass the top of the first pillar. Exceptions to this are Ca99 where the
i' is a little, and Cal 12, where it is distinctly surpassed by part of the mp^^).

') For the inconstancy of L in Hippuritinae, vide e.g.: Douvillé, H., 1910, Mem. S. g. F., 18, Mém. 41,
p. 12, ff. 8a—c (disappearance of truncature with age in V. dentatus)-. Kühn, O., 1932, Ree.'Geol. Survey
India, 66, 1, pp. 157, 158 (variability of L in Vacc. mdenburgi); idem, 1933, N. J. f. Min etc Bcil Bd 70B
pp. 241, 242 (id.).nbsp;. • • .

») This, of couse, is a very crude method. With regard to the variability of this feature cf. Douvillé H.
1910, Mém. S. g. F., 18 (xMém. 41), PI. 2, ff. 2, 2a, showing, how in V. tabumi the stem of the first pillar|
S, becomes thinner with age.

quot;) Palmer on p. 97 of the type description, says that the pillars are almost half as long as the L. On
the fig. 4 of his PL 5, this proportion appears to be about 2/3.

quot;) In the European samples it is alwap oblong and emarginate. Possibly, then, this is caused by the
comparative lowness of the sections, but it may be also a characteristic difference.

^i) It seems to me, that the „bquot; on fig. 4 of Palmer's PI. 5 does not represent the posterior tooth, but
the posterior myophore. The animal, should this be true, would belong to these exceptions, with internal
position of the posterior myophore.

These, then, conform to the sample of Toucas (textf. 172, Gosau) and
to that of Milovanovic (textf. 2, Leposavici).

The space of the circumference occupied by L—E, is also subject to
considerable variation; it is maximum 1/2,9 in Cal 15, minimum 1/5 in
Cal 02, 109. The distance L—S is about equal to that of S—E.

For a good appreciation of the variability a complete table of measures
and a goodish number of sections are given herewith.

Relation: Douvillé describes three distinct lots : 1. ? St. Wolfgang,
2. St. Gilgen amp; Oberberg, 3. Sirone. Those of the second lot are very
similar to ours as regards the ornamentation of the outer surface. They
agree furthermore with some of ours in having the top of the ligament,
not fully rounded. Douvillé considers them transitional between V. boehmi
and inaequicostatus. In accordance with this, only the pores near the margin
were seen to be complex in the Cuban material. The forms under discus-
sion differ from ours by the shortness of S, which is much shorter than
E, even more so, than in the other European samples. The L moreover is
straight. The inner margin of the outer shell layer is but feebly undulated.

The forms from Sirone agree with ours in having the inner margin
of the outer shell-layer distinctly undulated. They differ by the left valve,
which is depressed, even sunken in the Lombardian forms, elevated in ours.
Moreover the ornamentation is complex as in the typical form, and not
simple as in the Cuban material. L and E are straight or but a trifle curved.

As a whole the Cuban form is distinct from all European samples by
the elevation of the left valve, the characteristic ornamentation, and the
large Au—Piv V L angle. It is furthermore characterized by the undulation
of the outer shell-layer's inner margin, and the frequent deflection of L
and £ towards the anterior. In view of the enormous variability it is apparent,
that it cannot be specifically separated from inaequicostatus, but the differences
warrant its separation as a subspecies.

Age and faunal association: The stratigraphical position of the
typical form is not well settled as yet. At Sirone it occurs below Maestrichtian
layers with „Belemnites mucronatusquot; and therefore it was considered to
occur in the Campanian. According to Douvillé those from St. Gilgen
are of exactly the same age. Its association at Leposavici with V. boehmi,
oppeli, gosaviensis is noncommittal. As these related forms have a consider-
able vertical range, it might be possible that inaequicostatus too occurs in

Such cavities occur also in europcan forms, and have already been figured for instance by Woodward

Dcscribcd at the time (Douvillé 1897, p. 201) as „Campanien moyen . A similar item occurs at
p 205 f crès '1 Orbitoides du Campanien moycnquot;). Douvillé at the time included the Maestrichtian in the
Campanian as „Campanien superieurquot; (cf. p. 61). The „Campanien inferieur» of 1897 apparently applies
to the transitional strata between Campanian and Maestrichtian, or to the Lower Maestrichtian. Felix,
ignorant of this nomenclature, citcd Douvillé wrongly as an argument against De Lapparent s Maestrich-
tian age of the layers in question (Felix 1908, Paleontogr. 54, 6, p. 313).

-V

-f

a little
?

a little

a trifle
?

a trifle

little
little)
-f

-f

2,2
1,6

1.3
1,5

1.4

2.3

1.5
1,8

5.4

1.6

6.5
15

2.6
6,3
2,3
6

4,3
1,7
2,9

Explanatory : means : distinctly curvcd ; ant: towards the anterior side ; post : towards the
posterior side : A : with a triangular section ; emarg. : emarginatc ; obi. : oblong; trunc.: truncate.

A, emarg,

obi. emarg.
obi. trunc, ?
A

obi. trunc,

obi,
obi. trunc.

half

no
no
no

no
no
a little

a little

no
no
no

half
no
no

48
45
41
45
43
70

49
62
52

72
56

58
62
70
(46)
63

59
(60)

41
45
41
43

38
71

39
70

52
50

58
48

42
57

54
(60)

Explanatory : means : distinctly curved ; ant: towards the anterior side ; post: towards the
posterior side : A : with a triangular section; emarg. : emarginate ; obi. : oblong; trunc.: truncate.

48
45
41
45
43
70

49
62
52

72
56

58
62
70
(46)
63

59
(60)

41
45
41
43

38
71

39
70

52
50

58
48

42
57

54
(60)

A, emarg.

obi. emarg.
obi. trunc. ?
A

obi. trunc.

obi.
obi. trunc.

half

no
no
no

no
no
a little

a litde

no
no
no

half
no
no

no
a little
no

no
half
no

t) in a lower section: triangularly oval, truncate,
tt) in a lower section: oblong,
ttt) in a lower section: oblong.

15nbsp;20
20 19
13 12
18 18

16nbsp;15

20nbsp;19

15nbsp;15

21nbsp;22
24 17
18 16

16nbsp;10

21nbsp;14

33 28

22nbsp;19
30 22

13 14

gt;

2,2
1,6

1.3
1,5

1.4

2.3

1.5
1,8

5.4

1.6

6.5
15

2.6
6,3
2,3
6

4.3

1.7
2,9

2.8
7

2.4
6

1,3
1,3
11
1,1
1,7
1,7

( )
4-

a little
?

a little
a little

a trifle
?

a trifle

little

little)

older^ strata. On the other hand, a Hipp. (Vacc.) aff. inaequicostatus was
mentioned from the Syrian Maestrichdan by Vautrin, H., 1933 (Haut-
Commiss. Rép. fr. Syrie et Liban; Serv. trav. publ. ; Sect. étud. géol. ;
Notes et Mém., 1; I could not consult this paper). Cf also below, where
a new subspecies is described from the Cuban Maestrichdan.

At the same locality as the Cuban form are found : Torreites tschoppi,
„Pironaeaquot; corrali Palmer, Durania lope^-trigoi (Palmer) and D. curasavica
(Martin) and a Plagioptychine: ? Mitrocaprina sp. (p. 163). Vat „Pironaeaquot; for
reasons to be disclosed below, cannot be used as an argument. Dur. cura-
savica was found in Curasao together with Vaccinites ??iartini MacGillavry i^).
A Campanian (or even Maestrichdan) age was thought probable then.
Kuhn (1934, Pal. Zentr. bl., 4, p. 228) in his review of the paper in quesdon
considers a Campanian age of that fauna almost certain.

There is no doubt but that the Loma Yucatan and the Cura^aoan
Seroe Teintje fauna are of one and the same age. It is, then, of interest,
that in several slides, made through the bed-rock of either locahty, not a
single Orbitoid, nor a Camerina was found. As a result a Pre Maestrichtian
age is indicated. On the other hand, the presence of a Torreites here, and
that of a Vaccinites much related to the described form in the Maestrichtian
of San Diego de los Banos, show that the Yucatan fauna is related to the
Maestrichtian fauna.

Everything considered, there is a good agreement between the argu-
ments, and the fossils may be considered of Campanian age.

Vaccinites cf. inaequicostatus macgillavryi (Palmer).
1937 (Vaccinites sp.) Vermunt, L. W. J. — Journ. Pal. (in press), textfig. 2k.

A large, cylindrical sample from loc. H961, 1,5 km. S. of Central
Bramales, Pinar del Rio Province, Cuba (W. 12), pulled out of a coarse
conglomerate, which may be the basal conglomerate of the Maestrichdan.
Possibly its position there is secondary.

Diameter 74 by 74. Its ornamentadon is similar to that of the above,
but generally coarser. Vermunt gives a breadth of 2—3 mm for the ribs ;
it may attain, however, 5—6 mm. L and E are distinctly bent towards
the anterior side. The inner margin of the outer shell-layer is disdnctly
undulated. For the rest see the accompanying table. It is exceptional because
of the thickness of the L, the small value iotr\u (1 /5), and the small angle
An—Piv V ^ (30°). The distance L—S is greater than S—E (21 gt; 14), but
this is inside the range of variation of the subspecies.

A radial section through the left valve, again showed the complexity
of the pores. There are even complex pores more towards the interior.

Vaccinites inaequicostatus vermunti n. sbsp. (PI. 5, f. 2).
1937 (Vaccinites macgillavryi) Vermunt, L. \V. J. — Journ. Pal. (in press),

Three weathered right valves, all from Cuba: W 10 from loc. M 966,
3 km WSW. of San Diego de los Banos, Pinar del Rio Provmce, Cuba;
W 11 from loc. H 787, 0,5 km S. of the same town; the third, collected
by Dr. Tschopp, locality unknown. W 11 is chosen as type specimen.

W 11 has the left valve partly preserved, but a radial secdon was of
no avail. It showed that there is a large cavity under the anterior tooth in

The right valve is a low cone, with subcircular section. Ornamentation
unknown. Outer shell layer thick and infested with boring holes. Its inner
margin not undulated. The inner part of the inner shell layer consists of

forward or straight, club-shaped, pinched at the base. Of the same length
almost and of the same shape as E. E straight, not inclined. Dental appar-
atus as in the Loma Yucatan form, mp distinctly triangular in section.

It differs from the subsp. macgillavrji by the absence of undulations,
and by the straightness of E. From the European forms, and especially
from oppeli to which it comes nearest, it differs through the great angle
Aji—Piv\jL (40° amp; 50° here, 20° in oppeli), and by the first pillar's being

Because of the general similarity to the other form described I have
no doubt about its reladonship to that form, even though the nature of
the pores could not be established. The internal features however are much
like those of V. giganteus, which also has a large dental inclination i^). There
however, the second pillar is much longer than the first and the distance
L—S is much larger than S—E, the proportion r : // is smaller and the
posterior tooth distincdy surpasses the tip of the ligamental crest.

This species has been found together with Mitrocaprina palmen n. sp.
Age: Maestrichtian.

The European Pironaeae have been intensively studied in later years
by Milovanovic and Kuhn i^). They demonstrated, that the group of
Pironaea corrugata var. transitoria, corrugata, poljstjla var. slavomca etc. forms
a genetic entity. Its development has been stratigraphically and geograph-
ically traced. There is an almost continuous series of forms, and it is difficult

«) N B Vacmius mcmuus var. major Toucas was mentioned f'om Chiapas by F. K. G. Muellerried
(1933, GcoL Rundschau, 23a. Salomon-Calvi Festschrift, p. 270, and 1936, Bol. Soc. geol. Mex., 9. no. 1,

a. MiLOVANOVid, B.. 1934, Bull. Serv. géol. R. Yougoslavie 3, 2, pp. 65-151.
i. Kühn, O., 1935, Zentr. bl. f. Min etc.. B, 9, pp 353-368.
.. MiLovANOVié, B.. 1935. Geol. Balk., 1. 3 pp. ^0, 1^31
J. MiLOVANOVié, B., 1936, Ann. géol. Pén. Balk., 13, pp. 29-31.

Fig. 1. Parastroma guiiarti (Palmer). (Ca 129). Showing disconnected pillar-heads. x0,6.

Fig. 2. Vaccinites inaequicostatus vermunti n. subsp. Specimen collected by Dr. Tschopp. Natural size.

Fig. 3. Praeharrettia corrali (Palmer). (Ca 166). Note irregularity of pillars, emarginate mp and pseudo-canals. Natural size.

Fig. 4a-d. Torreites tschoppi n. sp. mp of respectively Ca 160, 161, 162, 163. Bevelled off, bicornous. Natural size.

Fig. 4e-h. Torreites sanchaz' (Douvillé). mp of respectively N 3, N 3 (lower section), N 1, Pa 303 1935. Bifid. Natural size.

Fig. 5. Parastroma guitarti (Palmer) juvenilis. Small specimen in colony Ca 127. Natural size.

Kig. 1. Mitrocaprina tschoppinbsp;quot;Note VMn\i\a and tacU-ward curvatuxe oï Mtrfco. TV\e tight -vaWc is only ^ust seen. 'Natural size.

quot;P'i.e.. ? MttTOcaIgt;rina sp.nbsp;quot;blote sVv^t omf-AepTessVon andnbsp;tootb. 3. tAo Piv' a\veo\c diffexervtVated. quot;NatMtaV sixe.

to find specified limits. Kühn could discern several forms, but since then, it
seems new intermediate forms have been found by Milovanovic (note 16d)
Anyhow as Kuhn remarks, (note 16b, p. 356) if a group of specimens from
one locality and from one niveau are distinctly centred round a defimte
and distinct type, it is better to name it, and exceptions must be left aside.

A parallel line to that of the European Pironaeae was observed m Persia.
A P. persica was described from this region by Vredenburg. This form
has strong undulations of the inner margin of the outer shell layer According
to Kuhn (note 16b, p. 363) these infoldings are also marked on the exterior.
This would mark an evolutional stage like that of P. corrugata. A transitional
form between this species and a more Vaccinites-X^quot;^^ type has been described
by Kuhn^') The undulations here are very weak, and for this reason,
it has been contended by Milovanovic (note 16a, pp. 69, 70), that this form
was not a real Pironaea, but a Vaccinites. The important side of the question
is that here a probably independent line of development is found, which
évoluâtes along the same lines, showing, that it is quite possible, that Pironaea
in a large sense is not a real genus, but a type of development.

Meanwhile several „Pironaeaequot; have become known from the New
World viz. : „Orbignyapacijicaquot; Olsson i^), P. peruviana Gerth, P. cf. peruviana
in Vermunt i^), and P. corrali Palmer 20). Now all these forms, with the
exception of P. corrali, have one point in common : the ratio r \ u h much
greater, than in all European forms. Even in P. corrali it is on the large
side, about 1 /5 and then, to judge from our material, which for the greater
part' is ill-preserved though, this angle is also larger in Palmer's species,
Ind his specimen is exceptional. The ratio is certainly large, about 1/3,
in our best preserved specimen, which is herewith figured (Pl. 5, f. 3).
Apparently these forms are subject to great variation in this respect. A
similar variability was observed in Praebarrettia sparcilirata by Thiadens 21):
not only the ratio L-S\S-E but also that oir-.u was found to vary
wildly Such exceptional forms as those of his fig. 2h, would almost certainly,
if found isolated, be indistinguishable from the more advanced European

MiLOVANOVié (note 16d, p. 30) gives a variation of 1/13 to 1/5 for the r : u
ratio of the var. slavonica group. On account of this, he thinks it impro-
bable that the American forms should have nothing to do with the
European ones, and he regards P. peruviana as intermediate between
Pironaea s. str. and Praebarrettia.

i7\ k-iViiM O IQ32 Rcc. ccol. Surv. India, 66, p. 160; textf. 3.
» SssoN A. a; im B^ll. Am. Pal., 69, pp. 48, 49; Pl. 8, ff. 1, 2.
» Vermunt, L. W. J., 1937, Journ. Pal. p«ss).nbsp;„ qr. pi 4 f 2

20 Palmer R. H., 1933, Rev. Agric. Habana, 14, nos. 15, 16, p. 98; Pl. 4 k. I.
In addition to à large number of specimens of P. corrali from the type locality, Loma Yucat^, Camaguey
Province Cuba our collections contain two other Cuban samples ofnbsp;One without locality,

conforms' lïern^y to the type described by Vermunt; externally it is cylmdr^al. The other from loc.

quot;) Thiadens, A., 1936, Proc. K. Ak. Wet. Amsterdam, 39, 8, pp. 1011—1013, textft. a , b—k,

Nevertheless, the fact remains, that the distance L—E, upon the whole,
is much larger in the American forms than in the European forms. And
this fact seems to be more or less independent from the stage of evoludon
reached. Thus, I am inclined to regard the American forms as a parallel
branch, developed independently from a centre of their own. This opinion
has already tentatively been expressed by Kuhn (note 16b, p. 365) 22). If this
is true, then the forms at hand would not be related to those of Europe,
and so the genus Pironaea would have to be regarded as a type of evolution,
or the American forms would have to be removed from it. There are some
other points of difference : the inclination of the dental apparatus seems
to be larger, and the diameter is smaller. Now it is of importance, that these
points, with the exception of the small diameter, are exactly the features,
which distinguish Praeharrettia from Pironaea. The best course to take, then,
will be to include all American „Pironaeaequot; in the genus Praeharrettia, even
though it is by no means certain, that Pr. sparcilirata is a descendant of
these forms. Should it be proved, that this is not the case, then it will
probably be better to make a new name for the Pironaea-X^e forms.

The rado r: uis± I/3 ; the inclination of the dental apparatus probably
is 50°.

Praeharrettia corrali (Palmer), (p. 123, f I; PI. 5, f 3; 10, f. 3).
1933 (Pironaea corralli) Palmer, R. H. — Rev. Agric. Habana, 14, nos. 15,

Numerous specimens (Cal65—195, several of them colonies) from the
type locality : Loma Yucatan, Camaguey Province, Cuba.

The of Palmer's figure does not represent the posterior tooth,
but the posterior myophore, which is triangular, truncate, even emarginate
in our specimen of PI. 5, f. 3 (Cal66). A typical feature of this species
is the irregularity of outline of all the pillars.

Structure: In a horizontal section a curious structure is observed. It
seems, as if numerous small canaliculi of about 0,2 mm breadth, traverse
the outer layer from its inner margin towards the outer surface, bifurcating
on the way. In a tangendal secdon, however, it is seen, that these supposed
canals run all along the entire length of the shell. Here they look like
longitudinal canals. In one tangential section, the original structure could
be observed. It appears, that the shell-growth was not continuous, but that
the outer shell layer is made up of „funnel-platesquot;, deposited at varying
distances. These are laid in a peculiar kind of folds. First a slack downfold

As Kühn (16b, p. 365) remarks, to check this supposition, it is first of all necessary to examine the
Spanish forms. This seems to have been done by Milovanovic (16d, pp. 30,31). They appear to be of the
European type, with a small r : u ratio, and very similar to some samples of P. polystyla var. slavonica.

is formed, then the plates rise steeply upward, to form a new slack downfold,
at a much higher level. Thereupon they turn downward again, steeply,
and form a new low-level downfold. At the steep places, they come into
contact with one another, and thus a certain firmness is secured. The low-
level downfolds correspond to the pseudo-canals of the horizontal section.
In the pillars, a very sharp and large upfold is formed by the plates, which
becomes less steep towards its sides. In accordance with this, one may
observe in a horizontal secdon, how the lateral parts of a pillar are continued
into a pseudo-canal towards the outer surface. In most specimens this
structure is obscured, and the plates have become invisible, but the zones
of high-level downfolds, where these plates turned back, downwards, at

the edges, retained a more compact aspect, whereas the zones of low-level
downfolds that are a mere prolongation of the direction at the edges,
became less compact. This explains, why these zones look like canals. In
a horizontal section it appears, that in the pillars a festoon-like folding is
superposed upon the main folding, described above.

1897nbsp;(Barrettia s.) Whitfield, R. P. — Bull. Am. Mus. Nat. Hist., 9,
pp. 245, 246 ; Pl. 36, 1 f ; 37, 1 f

1898nbsp;(B. monilifera var.) Douvillé, H. — Rev. crit. Paléoz., 2, 3, p. 125.

nos. 14, 15, p. 305.
1924 (Praeharrettia s.) Trechmann, C. T. — Geol. Mag., 61, pp. 395,

1932nbsp;(Barrettia s.) Boissevain, H. amp; MacGillavry, H. J. — Proc. K.
Ak. Wet. Amsterdam, 35, 10, pp. 1303—1308 ; textff. lab, 2ab, 3a.

1933nbsp;(Praeharrettia s. var. cuhensis) Palmer, R. H. — Rev. Agric. Habana,
14, nos. 15, 16, pp. 98, 99 ; Pl. 6, ff. 1, 2.

1935nbsp;MacGillavry, H. J. — Proc. K. Ak. Wet. Amsterdam, 38, 5,
pp. 562, 563. (Praeharrettia is to be included in Barrettia).

1936nbsp;(Barrettia s.) Thiadens, A. — Proc. K. Ak. Wet. Amsterdam, 39, 8,
pp. 1011—1013 ; textff. 2a, a', b-k; PI. f. 2.

1937nbsp;(Barrettia s.) Vermunt, L. W. J. — Journ. Pal. (in press).
Palmer (p. 99) considers Praeharrettia different from Barrettia on

account of the structure. It must indeed be stated, that the structure of
Barrettia is made up of three different items, as described by Whitfield :
in addition to the rays, which belong to the outer shell layer, and the tabulae,
which belong to the inner one, there is a system of tangential, vertical
walls, also belonging to the inner shell-layer. This latter system of calcareous
laminae seems not to occur in Praeharrettia. It is questionable, whether this
feature is of generic importance, and for this reason it has not been mentioned
in the key.

Two specimens collected by Dr. Tschopp (loc. Ts. 1429) 2,5 km NW.
of Ciego de Avila, may be reckoned to this species. Otherwise not recorded
from Camaguey Province.

Palmer (1933, I.e., p. 99 ; PI. 6, ff. 3—6) described another species of
this genus : P. porosa, from Sancti Spiritus, Santa Clara Province, Cuba.

Barrettia monilifera Woodward 1862.
1862 Woodward, S. P. — The Geologist, pp. 372—377 ; PI. 20, ff.
1-^: 21, f 5.

(1894 (Barrettia) Sapper, C. — Pet. Mitt., Erg.h. 113, p. 9.
1897 Douvillé, H. — Mém. S. g. F., 7 (Mém. 6), p. 230 ; textf. 66.
1897 Whitfield, R. P. — Bull. Am. Mus. Nat. Hist., 9, pp. 233—244 ;
textff. on pp. 241, 242; Woodward's figures reprinted; PI. 27,
ff 1,2 ;28,f 1 ;29,f 1 ; 30, f. 1 ;31,f 1 ; 32, f 1 ; 38, ff 1—4. 24)

quot;) These authors consider Barrettia related to the Hippurites biomlatus group, i. e. to Hippurites s. str.,
and expcct it to have linear pores.

Whitfield, p. 232, note 2, citcs a number of authors, who doubted the bivalve nature of this fossil
(Zittel, Tryon, Linstrom).

1899nbsp;(Barrettia) Sapper, C. — Erg.h. 127 zu Pet. Mitt., Em. Bd. 27
pp. 39, 66.nbsp;amp;nbsp;.

1901 (Barrettia) Sapper, C. — Mitth. Geogr. Ges. Hamburg, 17, p. 87.
(1901 (Barrettia) Hayes, C. W., Vaughan, T. W. amp; Spencer, A. C. —
(pp. 24, 34 in Ortega's reprint of 1918).

1903nbsp;(Orbignya m.) Toucas, A. — Mém. S. g. F., 11 (Mém. 30), p. 47 •
textf 73.nbsp;23)

1904nbsp;Douvillé, H. — Rev. crit. Paléoz., 8, 3, p. 182.nbsp;23)
*(1919 (Barrettia) Vaughan, T. W. — Smithsonian Inst., bull. 103, p. 547.

1921nbsp;Klinghardt, F. — Die Rudisten, 4, Pl. 16, ff. 3 4-18 f 22 •
23, f. 3.nbsp;' . . ,

1922nbsp;(B. cf. monilifera) Trechmann, C. T. — Geol. Mag., 59, pp. 510
511 ; Pl. 19, ff. 2ab; 20, ff. 1, 2.nbsp;0 rr gt;

nos. 14, 15, p. 305.
(1926 Sanchez y Roig, M. — Soc. Geogr. Cuba, p. 11.
(1926 (B. sparcilirata, B. monilifera) Douvillé, H. — C. R. S. g. F., p. 71.
1926 (B. monilifera, Prebarrettia sparcilirata) SAnchez y Roig,'m. —

Mem. Soc. Felipe Poey, 7, pp. 95, 96, 98, 99 ; Pis. 2-^.'
1926 (B. sparcilirata, B. monilifera) Douvillé, H. — B S e F (4) 26
pp. 128, 129 ; Pl. 7, ff. 1, 2.nbsp;• • b- v ; ,

1935nbsp;Mac Gillavry, H. J. — Proc. K. Ak. Wet. Amsterdam 38 5
pp. 558, 559.nbsp;' '

1936nbsp;Rutten, M. G. — Journ. Pal., 10, 2, pp. 135, 136.nbsp;25)
(1936 Muellerried, F. K. G. — An. Inst. Biol. Mexico, 7, 1, pp. 155—164.
(1936 (Barrettia) Muellerried, F. K. G. — Bol. Soc. geol Mex 9*

In Camaguey Province, this fossil occurs at several localities :
Arroyo Hondo (Douvillé, SAnchez, our collecdons : Cal 54—157),
loc. L 702, L735 (both on the Carretera Central West of Camaguey city)'
San Jose de los Jibaros (Lopez Trigo don.).

With the exception of Cal 54, which was collected more to the West
(loc. L662), all samples of Arroyo Hondo are at variance by the wide
spaces between the rays, and between the beads of one ray. Those near
to the diorite became secondarily silicificated.

The material does not warrant any further remarks. A large number
of these unwieldy fossils will have to be studied to settle the question of
the specifical limits of the different species of the genus Barrettia.

quot;) Wrongly citcd by Muellf.rriud (1936, An. Inst. 13iol. Mcxico, 7, 1, p. 156): Rurria^ did not unite
the spccics spcrdUrata with monilifera, but only the „sparcilirataquot; of Douvillé and SAnciifjc, which had
already been separated from Whitfield's sparcilirata by Boissevain and Mac Gillavry (1932 Prix: K
Ak. Wet. Amsterdam, 35, 10, pp. 1304, 1306, 1307).

1897nbsp;Whitfield, R. P. — Bull. Am. Mus. Nat. Hist., 9, p. 244 ; PI. 33,
f. 1 ; 34, f. I ; 35, f. 1.

1898nbsp;Douvillé, H. — Rev. crit. Paléoz., 2, 3, p. 125 („5. jjiultilirata
et B. sparcilirata nous paraissent être de simples variétés de
B. monilifera''').

1921nbsp;Klinghardt, F. — Die Rudisten, 4, Pl. 16, f. 6 (= Whitfield's
Pl. 33).

1922nbsp;(cf. multilirata) Trechmann, C. T. — Geol. Mag., 59, pp. 511
512 ; 19, f. 1.

(cf. multilirata var. conica) id. — p. 511 ; Pl. 18, IF. lab.
(cf. multilirata var. cjlindrica) id. — p. 511 ; Pl. 20, f. 3.
1926 Sânchez y Roig, M. — Mem. Soc. Felipe Poey, 7, pp. 96—98 ; Pl. 5.
(1936 Rutten, M. G. — Journ. Pal., 10, 2, p. 135.
1937 Vermunt, L. W. J. — Journ. Pal. (in press.)

This species has not been encountered in Camaguey Province. It
remains still to be proved, that it is indeed specifically distinct from monilifera.

A bibliography and synonymy of the two species of this genus has
been given in a former paper (1935, Proc. K. Ak. Wet. Amst., 38, 5, pp.
599, 560).

(1936 (Parastroma sp.) Rutten, M. G. — Journ. Pal., 10, 2, p. 135.
1936 (P. sanche^i) Thiadens, A. — Proc. K. Ak. Wet. Amsterdam, 39,
8, p. 1013 ; Pl., f 1.
The type locality is Arroyo Hondo, Camaguey Province, Cuba. One
specimen in our collection was found at the same place (loc. L 662, Cal 47).
Sanchez's specimen from „Finca Quesadaquot; (probably near to Arroyo
Hondo).

Palmer's material was found near Sancti Spiritus (cf. Palmer 1933,
Rev. Agric. Habana, 14, nos. 15, 16, p. 96, unàet P. guitarti : „Esta espccie
junto con 0. sanche^i. .quot;). The material of Rutten and Thiadens was
found in the same Province at the localities H 156, 10 km W. of Santa Clara
city and at L 549, 550, 553, 554, about 12 km NW. of Cabaiguan. At L 549
the species was associated with Pseudorbitoides and Camerina dickersoni.

The type locality is Sancti Spiritus, Santa Clara Province, Vermunt's
specimen is from San Diego de los Bafios, collected by Dr. Tschopp. The

M 840 and Cal 30, 131 from the Eastern continuation of the Ingenio Grande
zone at loc. AI874.

The genus as such is fully defined in the key, and by the figures of
P. gmtarti. It is indeed a Barrettia with the rays, L and the stems of and E
entirely effaced. It is furthermore remarkable by its large size and the large
size of the teeth.nbsp;^

P^ guitarti is covered externally with large, more or less triangular
ribs The angle ^v^/F is about 180°. The mp is shorter than the two
teeth. The umbo of the right valve is often somewhat excentrical nearer
to the side opposite Some of the large specimens are slightly curved
and give the impression of having laid, cucumber-like, upon the sea-floor'
Associated with Orbitoids (Cal 20, 136), Vaughamna (Cal 37), Camerina
dickersom (Cal26, 136, 137) and Miliolids (Cal36, 137). Some of them give
evidence of having formed a couple with another of their own kind Cal 27
is a colony of small specimens. An extremely young sample was observed
m a section through this colony. It gives the impression of being Pironaea-
like in having distinct infoldings of the outer shell-layer (PI. 5 f 5) It is
impossible, though, to be sure of this, as no slide could be made Often
at the mner margin of the outer shell layer rudiments are indeed found of
such infoldings In one interesting sample these are a little longer than-
usual, and distinctly moniliform. This, then, would be a form of passage
between Barrettia and Parastroma.

The two species are characterized by their structure. That of P. mitarti
(PI. 10, ff. 7—9) consists mainly of tabulae. Seen in a radial section these
tabulae are thrown into a series of sharp folds, which become narrower
towards the periphery. The upfolds are almost always open, so that the
tabulae apparently are not continuous. Each downfold is fitted with a
sharp keel, which does not reach the tabula below it, but stops short
near to it. In these downfolds the shell-deposition may be continuous
and the bottom of a fold is compact with numerous parallel growth-lines'
while the keel of the downfold above it, presents itself as a median line!
This compact area thins out towards the adjoining upfolds. In one place
a compact area was found between two upfolds. This is one of the few
cases where an upfold is not open. In horizontal sections the structure
appears to be mainly concentrical, but slight tangential undulations of
niveau bring into view the same features as seen in a radial section,

»•) Sometimes there arc no real infoldings of the outer shell layer, but only sharp upfoldings of the
tabulae, radially directed and marginal, proceeding a little way towards the interior. They may mark the
placcs, where in a former stage were situated the rudimental infoldings.

accordingly lengthened. The keels may be distinctly seen in several places.
A tangential section does not differ from a radial one, owing to its not
being concentrical. In the middle, where this direction is nearly approx-
imated, the tabulae are seen to lie nearly horizontally one above the other.
At the outside of worn specimens, the tabulae appear to have flat-bottomed
downfolds in a tangential sense, with sharp upfolds, where an infolding
of the outer shell-layer occurs (cf. note 26). These folds - do not reach
far into the interior and mostly stop, where the infolding send. That's why they
are not seen in the tangential section. In a horizontal section they present
themselves as a peripheral zone of rectangles. Often there are more than
one zone of rectangles in a radial direction, showing that the peripheral
radial upfold has cut through one of the concentrical folds described
above. In that case, the infoldings of the outer shell-layer are prolonged
by zig-zag lines, separating the adjoining rectangles from one another.

In P. sanche^i (PI. 10, ff. 10—12) the structure does not differ in prin-
ciple, but here everything is much smaller. Moreover, the structure is no
longer concentrical or only obscurely so, and the upfolds and downfolds
alike are conical. They are most irregularly distributed, only faintly arranged
in zones (cf Thiadens, p. 1013 ; PL, f. 1), and very numerpus. Again
the upfoldings are open at the top, but now, because of the conical nature
of these upfolds, the tabulae are continuous but for the holes in the fold-
tops. The downfolds again are fitted with keels, not reaching the tabula
below, but here the keels are more reduced. If in the figures of the radial
and tangential section, the different tabulae are projected into one tabula,
we see as in a film, the nature of the folds.

The specimen from Pinar del Rio is interesting, because it shows in
places a puckering or a folding of the tabulae across the usual concentrical
direction of folding. Thus it marks already a tendency towards a more
complicated structure, an inclination towards a sanche:(j-Y]kQ. structure.

There is still much to be investigated about this interesting genus.
For instance, whether there is really a slit in the left valve through which
the L passes, as is the case for the two pillars ; whether the L changes its
length and breadth with age, or not; more should be known about the
structure of the outer shell layer of the left valve ; further it should be of
interest to study extremely young samples of this genus. Our matenal is
much too scant for such studies.

Torreites sanche:(i (Douvillé). (PI. 5, ff. 4e—h).
1927 (Hippurites (Vaccinites) Sanche:(i) Douvillé, H. — B. S. g. F., (4) 27,

pp. 54, 55 ; PI. 4, f. 1.
1933 (Torreites, Torreites sanche^i) Palmer, R. H. — Rev. Agtic. Habana, 14,
nos. 15, 16, pp. 99, 100 ; PI. 7, ff. 1, 2 ; 8, ff. 1, 2.

1935nbsp;(Torreites) Mac Gillavry, H. J. - Proc. K. Ak. Wet. Amsterdam
38, 5, pp. 563, 564.

The species has been found in the following localities : Arroyo Hondo
Camapey Province (type locality); H550 (N. of Anton Diaz), M557
(N. of Anton Diaz), L 543 (Bernia) in Southern Santa Clara; H 870 (Verra-
cos) in Pinar del Rio Province. All in Cuba. Palmer does not mention
where his material has been found. No material was collected by us in
Camaguey Province.

Five groups (Cal 60-164) of respectively 3, 1, n, 1,'2 specima, of a new
yecies of this genus, were found at loc. V529, Loma Yucatan, Camaguey
Irovince, Cuba. Evidently a colonial species. The colony of three (Cal60 -
two larger and one young specimen) is chosen as type colony.

A much smaller species. Most specimina have a diameter of about 40 mm
u ^nbsp;'' '^^stincdy greater : 69 by 55 mm. The species sanchezi on the

other hand has an average diameter of about 90 to 100 mm. The outer surface
of the left valve is almost entirely flat in some samples, in others not. Its
surface is entirely feature-less. On the inside it bulges downward between
and beyond the pillars and L. Its structure as in sanche^i. For the rest also
It is much like that species. It differs in the following points The outer
surface of the right valve of sanche^^i is covered with large, rounded low
ribs between the infoldings ; that of this species is merely costulate' the
nbs at a distance of 1—2 mm. There are no infoldings in its outer shell layer
The angle between L and E, though very vanable in both species, constitutes
another difference. It vanes from 45—70° in tschoppi, from 75—120° in
saNchezi, but in an exceptional case of the latter spccies it was found to be
50°. The mp constitutes another difference, it is bevelled-off, bicornous
in tschoppi, bifid in saficheii (cf Pl. 5, 4 a-d, 4 e-h). The pillars and
L are more irregular in shape, but the main theme is not different from
that of safiche^i, i. e. they are broad and long and of uniform breadth
from base to top. L is extremely long, J is a litde shorter and E is quite
short. In accordance with the small size, the breadth of L and pillars is
smaller. So a maximum breadth of 2 mm was found for the L oitschoppi to
a minimum breadth of 5 mm for the L of smche^i.

The species is characterized by the lack of infoldings, the smallness
the costulation of the right valve's outer surface, and the bicornous mb
This spccics is named in honour of Dr. Tschopp.

Amphitricoelus waringi Harris amp; Hodson, 1922.
1922 Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer., 1, pp. 130—133 ;

PI. 18, 1 f ; 19, ff. 1—6; 20, ff. 1—5; 21, ff. 1—11 ; 22, ff 1, 2.
Age: „most likely a Cenomanian horizon, though it may be as low as

Aptianquot;. (Harris amp; Hodson, p. 133).
Loc.: Near Plum Road, just south of the 51/4 mile post, eastern part of
Trinidad.

Many fragments from Plum River, Trinidad, in the Naturhistorisches
Museum in Basel, collected by Kugler, identified by Bouwman
and me.

1899nbsp;Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico, 2, pp. 147,
148 ; textff. 15, 16 (same text and figs, as in 1898).

Age: „Upper Cenomanianquot; (Boehm, resp. p. 332 and 154) ; „Cenomanianquot;

According to Palmer this animal might be a Planocaprina (Palmer,
1928, p. 67). A new light is thrown upon this form by the work of Palmer:
because of our present knowledge, it is certain, that the figs. 2, resp. 15 do
not represent a left valve at all, but, on the contrary, a right valve, seen
from the apex towards the commissure, i. e. not in the usual orientation,
but reversed. In this way the „0Z)'quot; does not represent a cavity in the
anterior tooth 2), but the alveole An of this tooth. „«quot;' is not the accessory
cavity, but the P/k' -f omp' cavity. Seen like this the animal has canals in
both valves, with the walls mostly simple or bifurcating, seldom polyfurc-
ating. It has the two ribs, that are frequent in Coalcomana and Caprinuloidea
(cf Thiadens, A., 1936, Proc. K. Ak. Wet. Amsterdam, 39, 9, pp. 1135—

t) The age of the species is given as in the literature. For the writer's personal opinion on the age
of some species see pp. 10—12.

1) Burckhardt, C, 1930, Mém. Soc. Pal. Suisse, 49/50. As Burckhardt's work lacks an index, wc
give here, for the reader's convenience, the pages, on which a Mexican species is mentioned.

») Cavities in the anterior tooth do occur in Sahinia kiigleri for instance, but it is not clear, whether this
is primary, or secondary, caused by dissolution.

1140), one at the anterio-ventral corner, the other at the ventral corner
Apparently it is a form closely allied to Coalcomana, but with the canal-walls
much simpler, i. e. a Planocaprina.

1852 Roemer, F. — Die Kreidebildungen von Texas, etc., Bonn n 79 •
PI. 5, ff. 6a-f.nbsp;'

1888 (Ichthyosarcolites c.) Roemer, F. — Pal. Abh., Dames amp; Kayser
4, 4, pp. 10, 288.nbsp;'

foss. Inv., 1, p. 549 ; textff. 752ab.
(1926 (Ichthyosarcolithes? (Caprinula) c.) Scott, G. — thesis, Grenoble
p. 172.

(1928 (Caprinula (?) c.) Adkins, W. S. — Bull. Univ. Texas, 2838, p. 146.
Age: „Upper Albian or perhaps rather the base of the Cenomanianquot;
(Douvillé 1898, B. S. g. F., (3) 26, p. 387); „Edwards limestone,
Fredericksburg division (intermediate layers between the Rudist-
bearing strata of the Lower Albian found in the Pyrenees and those
of the Upper Albian of Portugal. Or in Jacob's stratigraphy : strata
with Mortoniceras hugardianum and Hoplites dentatusquot; (Scott, p. 176) ;
„near the top of the Middle Albian (Adkins, 1930, Bull. Univ'
Texas, 3001, p. 77).

Loc.: Waco camp on the Guadalupe, above New Braunfels Texas*
Upper course of Pedernales River ; San Saba River, Texas (Roemer
1852, p. 79). Adkins, p. 146 : Central Texas.

Caprina guadalupae Roemer 1849.
*1849 (Caprina Guadalupae) Roemer, F. — Texas, Bonn, p. 408.
1852 (C. G.) Roemer, F. — Die Kreidebildungen von Texas etc

Bonn, pp. 79, 80 ; PI. 5, ff 4ab.
1926 (Ichthyosarcolithes ? (Caprina) g.) Scott, G.—thesis, Grenoble, p. 173
1928 (Caprinula (?) g.) Adkins, W. S. — Bull. Univ. Texas 2838, p. 146
Age: as for the preceding species: „Together with Caprina crassifibraquot;.

Caprina occidentalis Conrad 1855.
1855 Conrad, T. A. — Proc. Ac. Nat. Sc. Philad., 7, p. 268.
*1857 Conrad, T. A. — Rep. U. S. and Mex. Boundary Surv., Washington

*1909 (Caprina occidentalis) Grabau, A. W. amp; Shimer, H. W. — North
Am. Index foss. Inv., 1, p. 549; textff. 753a—c.

(1926 (Ichthjosarcolithes ? (Caprina) o.) Scott, G. — thesis, Grenoble, p. 173.

(1928 (Caprinula (?) occidentalis) Adkins, W. S. — Bull. Univ. Texas,
2838, p. 146.

Loc.: type locality: „near the mouth of the Puercos River, Texasquot;; for
Boehm's material see Caprinuloidea whitei.

The preliminary description of 1855 is entirely insufficient. I could not
consult the description of 1857, but according to Boehm (resp. p. 325 and
146) there also the fossil is „ganz ungenügend dargestelltquot;. So we must
put Conrad's species aside as a problem and treat Boehm's material seperately.

This material was identified by Ch. A. White (in litt.) as C. occidentalis.
This identification was accepted by Boehm on the autority of White, but
with some reserve, and the name ,, Whiteiquot; was reser^^ed for it just in case.
In the present paper, the material will be referred to under this name (vide
Caprinuloidea whitei (Boehm)).

Now just as in Caprina cf. adversa the fig. given does not represent a left
valve but a right one, seen towards the apex this time, i.e. in the usual orien-
tation. Thus must be struck, while „«quot;' indicates thenbsp;alveole,
this time. Towards the ventral side the apparently curved valve is cut tangen-
tially, so that the canals to the extreme right in the figure are a reiteration of
those to the left. So we do not know, whether ventrally, ribs are present. The
canals are polygonal and radial. Dorsally the walls divaricate. The Pjv' -f
-f omp cavity is not like that of Caprinula (cf Adkins, p. 82: Caprinula sp.),
but like that of Caprinuloidea. Apparendy the form belongs to the latter
genus, hence the name Caprinuloidea rvhitei (Boehm) (see p. 137), whither
may be referred for age and locality, etc.

*1904 Stanton, T. W. in Ransome, F. L. — Prof Pap., 21, U. S. Geol.
Surv., p. 70.

*1857 Conrad, T. A. — Rep. U. S. amp; Mex. Boundary Surv., Washington,
1, 2, p. 147; PI. 2, fF. 2ab.

(1926 (Ichthjosarcolithes ? (Caprina) p.) Scott, G. — thesis, Grenoble,
p. 173.

According to Roemer, possibly the „other (straight) valve of C occi-
dentalisquot;.nbsp;quot;

1922 Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer., I on 134 135 •
Pl. 25, 7 ff.; 26, ff. 3, 4.nbsp;' ' FF , ,

If the orientation of the right valve is correct, these fossils would cer-
tainly have an omp of European type (see later), with subdivided omp, and
small oma canals, and then the animal might well be a real Caprina, However:
„much better material must be secured and worked out, before the generic
position of this species is well determinedquot; (Harris amp; Hodson, pp. 16, 17).

Caprina quadrata Conrad.
1855 Conrad, T. A. — Proc. Ac. Nat. Sc. Philad., 7, p. 266.
Age: „Cretaceousquot; (Conrad, p. 265).
Loc.: Alabama.

Caprina ramosa G. Boehm, 1898, vide Coalcomana ramosa.
Caprina (?) texana Roemer, 1849, = „Toucasia texanaquot;.

1899nbsp;Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico, 2
p. 148; textf 18 (same text and fig. as in 1898).

?(1899 (Schiosia sp.) Felix, J. — Felix amp; Lenk, Beitr. Geol. Pal Ren
Mexico, 2, p. 172.nbsp;^'

Said to be a left valve. The animal belongs to one of the following
genera: Caprintdoidea, Caprinula, Sphaerucaprina or Mitrocaprina, but not to
Caprina, for it has polygonal canals. The generic position is uncertain, as
the posterior muscle attachment of the right valve is not known. Ligament
unknown. Mitrocaprina is improbable because of the fossil's age.

Caprina ? in Heilprin 1890.
1890 Heilprin, A. — Proc. Ac. Nat. Sc. Philad., p. 469; Pl. 13, f 7.
Age: „Cenomanianquot; (Burckhardt, p. 199).
Loc.: Cerro de Escamela (Heilprin, p. 461), Mcxico.
No description, figures insufficient.

Caprina sp. indet. in Meek 1870.
*1870 Meek, F. B. — Proc. Am. Philos. Soc., Philadelphia, 11, p. 429.
Age: „Cretaceousquot;.

It is clear from the above, that the occurrence of the genus Caprina in
America remains yet to be proved._ C. phmensis seems to come the nearest
to the generic definition, but even there a lot of uncertainty is involved.

Caprinula anguis (Roemer).
1888 (Ichthjosarcolites anguis) Roemer, F. — Pal. Abh. Dames amp; Kayser,

4, 4, pp. 287, 288; PI. 31, ff. 7ab; 32, ff. 2a—d.
1898 (Caprinula) Douvillé, H. — B. S. g. F., (3) 26, p. 388.
• 1900 (Caprinula anguis) Douvillé, H. — B. S. g. F., (3) 28, pp. 220, 221 ;

Age: „Upper Albian or perhaps rather the base of the Cenomanianquot;
(Douvillé, 1898, B. S. g. F., (3) 26, p. 387); „Edwards limestone,
etc.quot; (cf Caprina crassifibra) (Scott, G., 1926, thesis, Grenoble);
„Vraconnienquot; (Upper Albian) (Douvillé, 1927, B.S.g.F., (4) 27, p.51).
Loc.: Two miles above the mouth of Barton's Creek, near Austin, Texas
(type locality) (Roemer, p. 281); „Of more common occurrence
(Hill, R. T., 1901, 21th Ann. Rep. U. S. geol. Surv., 7, p. 240);
Crawford, Texas (Adkins, W. S., 1928, Bull. Univ. Texas, 2838,
p. 146). (Not Austin-Chalk as was said by Roemer).
Roemer gives only an insufficient figure of the right valve. The canals
are visible, but not the muscle attachment. Moreover the figures of the
left valve were demonstrably wrong (cf. I)ouvillé 1900). Douvillé could
not retrace the original types of the right valve, only those of the left valve,
so that we cannot be sure, whether the species belongs to Caprinula, Caprinu-
loidea or Sphaerucaprina. On the whole the canal pattern of the left valve,
especially outside the f?ia is more rerniniscent of that of Caprinuloidea, than
of the other two genera. In accordance with this the canals of the right
valve, according to Douvillé (p. 221) are tabulated (cf. Caprinuloidea septatd),
as seen in some fragments.

Caprinula cfr. anguis in Adkins 1930.
(1930 Adkins, W. S. — Bull. Univ. Texas, 3001, p. 82.)
Age: not much later than Middle Albian CMuir, J. M., 1936, Geol.

») d'ORBiGNY, 1847, Ann. Sc. nat., (3) Zool., 8, pp. 261—263, ncc Terr. crét. as in Kutassy, 1934,
Foss. at., 68, p. 158.

Caprinula cubensis Douvillé.
1927 Douvillé, H. — B. S. g. F., (4) 27, pp. 52, 53; textf. 1.
*1930 Sanchez y Roig, M. — Mem. Inst. Nac. Invest, cient., p. 131
From Arroyo Hondo, Camaguey Province, Cuba. Vide pp. 73, 82:
? Antillocaprina cubensis (cf. A. annulata).

Caprinula (?) occidentalis (Conrad) 1855, vide Caprina occidentalis
and ? Caprinuloidea whitei (Boehm).

Caprinula quatuoralata Palmer.
1933 Palmer, R. H. — Rev. Agric. Habana 14, nos. 15, 16, p. 102 ; PI 3
ff. 3, 4.

Caprinula sp. in Palmer 1928.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, p. 71 ; PI. 13, f i.
(Burckhardt, p. 296).
Age: „Cenomanianquot; (Palmer, p. 24).
Loc.: Paso del Rio, Colima, Mexico.

An unidentifiable fragment with tabulated canals. It might quite as
well represent some Antillocaprina-Wkz fossil.

Caprinula 2 spp. in Adkins 1930.
(1930 Adkins, W. S. — Bull. Univ. Texas, 3001, p. 82.

Caprinula is further mentioned by Palmer 1928 (Occ. Pap. Calif Ac.
Sc., 14, p. 71): „this genus is well represented in different parts of Mcxico,
as many fragments from widely separated localities bear witness. It is to
be regretted, however, that no complete or even nearly complete specimens
are thus far foundquot;.

It will have become clear, that it is altogether uncertain, whether the
genus occurs in the Western Continent at all.

Caprinuloidea bisulcata Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif. Ac. Sc., 14, p. 64 ; PI. 12, ff. 1,2.
(Burckhardt, p. 208).

Caprinuloidea costata Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif. Ac. Sc., 14, pp. 62, 63 ; Pl. 11

According to Palmer, p. 63, this species may be identical with Coal-
comana ramosa (sic!). On Palmer's PI. 11, f. 5, there are indeed scarcely
any polygonal canals, ventrally This is also the case in some specimens
of this species, in the Basel Museum, collected by T. Keller at Caracoles,
S. Jalisco, Mexico. Polygonal anterior canals are present in this species,
but so are they in Coalcomana, cf Douvillé (1900, B.S.g.F., (3) 28,
textff. 1—4). All considered the species belongs not to Caprinuloidea, but
to Coalcomana, identical with ramosa, or differing from it on account of
the exterior.

Caprinuloidea multituhijera Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif, Ac. Sc., 14, pp. 61, 62 ; PI. 10, f 2.
(Burckhardt, p. 208).
Age : „Cenomanianquot;.

Caprinuloidea perfecta Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif. Ac. Sc., 14, pp. 59, 60 ; PI. 8

f. 8 ; 9, ff. 1,2; textf. 6.
1936 Thiadens, A. — Proc. K. Ak. Wet. Amsterdam, 39, 9, pp. 1134—

Age: „Cenomanianquot; (Palmer, p. 24); „Cenomanian-Turonianquot; (Thia-
dens, p. 1133).

Loc. : Soyadan de Adentro, Jalisco, Mexico (type locality); Southern
Santa Clara, Cuba (loc. A 236, near Matagua; cf. Thiadens, I.e.,
textf. 1).

Caprinuloidea perfecta subsp. gracilis Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 60, 61 ; PI. 9

On PI. 10, f. 1, „posteriorquot; stands for posterio-ventral; „ventralquot; for
the anterio-ventral side.

«) Palmer's description: „a well defined inner row of peripheral canals is present between the un-
branched radial plates. The plates regularly branch three times on the ventral side and once or not at all
on the dorsal sidequot; does not make sense. Perhaps, „peripheralquot; is a lapsus for polygonal, but then it would
not be truenbsp;i /o .

1928 Palmer, R. H. — Occ. Pap. Calif. Ac. Sc., 14, p. 62 : Pl. 9 f 4 •
10, f 3; 11, f. 1.nbsp;^nbsp;' • '

1898nbsp;(Sphaerucaprina occidentalis, respectively Jquot;. Whitei) Boehm G —
Z. D. g. G., 50, pp. 324, 325 ; textf. 1.

1899nbsp;(id.) Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico, 2,
pp. 145, 146 ; textf. 12 (same text and fig. as in 1898).

(1930 (Caprinula sp.) Adkins, W. S. — Bull. Univ. Texas, 3001, p. 82.
Age: „Not much later than middle Albianquot; (Muir, J., 1936, Geology

of the Tampico Region, Mexico, Am. Assoc. Petrol. Geol.).
Association : with Eoradiolites aff. quadratus (cf Adkins, 1930, Bull. Univ.
Texas, 3001, p. 82) (= „Sauvagesia spquot; in Boehm, 1898, Z.D.g.G.,
50, p. 325 ; 1899, Felix amp; Lenk, Beitr. etc., 2, pp. 146, 147 : textff
13a—c).

Loc. : Choy Cave, between Las Palmas and Taninul on the Tampico-San
Luis Potosf railway, San Luis Potosi, Mexico (cf Adkins 1930
Bull. 3001, p. 82).

For a justification of the name used here, see p. 132. The species
belongs in the neighbourhood of C. multitubifera.

Age: „Cenomanian-Turonianquot; (cf. Thiadens, I.e., p. 1133).
Loc.: Southern Santa Clara, Cuba (loc. A 236, near Matagua; L328,
E. of Matagua; vide Thiadens, I.e., textf i).

? Caprinuloidea anguis (Roemer) 1888, cf. Caprinula anguis.
Maybe a Caprinuloidea related to multitubifera. As the right valve is not
sufficiendy well known, one cannot be certain whether the generic deter-
mination is correct.

? Caprinuloidea felixi (Boehm) 1898, cf Sphaerucaprina felixi Boehm.
As the right valve, is not known, we cannot be sure about the right
genus. The ligament is that of a Caprinid. If the animal turns out to be a
Caprinuloidea it will be found to be closely related to multitubifera.

? Caprinuloidea lenki (Boehm) 1898, cf Sphaerucaprina lenki Boehm.
Again no right valve is known. Neither is the ligament. There are
but few polygonal canals in this species.

? Caprinuloidea sp. (Boehm) 1898, cf. Sphaerucaprina sp. Boehm.
No right valve known. Canal-pattern with numerous polygonal canals,
cf. multitubifera. Ligament not known.

? Caprinuloidea sp. (Boehm) 1898, cf. Caprina sp. Boehm.
Right valve and ligament not known. Generic position therefore
uncertain. If a Caprinuloidea, then cf. multitubijera.

? Caprinuloidea sp. (Heilprin) 1890, cf. p. 59: Ichthjosarcolites? Heilprin.
A Caprinid with polygonal canals. Insufficiently described and figured.

? Caprinuloidea sp. (Heilprin) 1890, cf. Caprina ? Heilprin.
No description. Figures insufficient. Possibly a right valve?

Coalcomana Harris amp; Hodson 1922.
For the difference between this genus and Schiosia cf. p. 148 note 16).

Coalcomana costata (Palmer) 1928; for discussion and bibliography cf:
„Caprinuloidea costataquot;. This species may be identical with Coalcomana ramosa.

1899nbsp;(Caprina r.) Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep.
Mexico, 2, p. 148 ; textf. 17 (same text and fig. as in 1898).

1900nbsp;(Schiosia r.) Douvillé, H. — B. S. g. F., (3) 28, p. 206 ; textff. 1—7.
1922 (Coalcomana r.) Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer.,

1, pp. 130, 132 ; PI. 6, ff. 4—7.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 62,69; PI. 12, ff. 3,4.
1936 Thiadens, A. — Proc. K. Ak. Wet. Amsterdam, 39, 9, p. 1140 ;

(in Thiadens, I.e., p. 1133).
Loc.: Cerro de Escamela, Orizaba, Vera Cruz, Mexico (type locality)
(Boehm, I.e., p. 325 and p. 147); Coalcoman, Michoacan, Mexico
(Douvillé, 1. c., p. 209); Soyatlan de Adentro, Jalisco, Mexico
(Palmer, 1. c., p. 69); Southern Santa Clara, Cuba (loc. M 656, near
Fomento; loc. L58 amp; 59, near Cruces; cf Thiadens, p. 1140
and textf. 1).

For the possible identity of Coalcomana costata with this species vide
p. 136 : „Caprinuloidea costata'\

? Coalcomana felixi (Boehm) 1898, vide „Sphaerucaprina jelixr and
? Caprinuloidea felixi. According to Palmer (1928, Occ. Pap. Calif. Ac. Sc.,
14, p. 62) this species might belong to Coalcomana, but as it has distinct
polygonal canals, ventrally, this is hardly possible. Caprinuloidea is more
indicated.

Planocaprina Palmer 1928.
N.B. Adkins (1930, Bull. Univ. Texas, 3001, p. 77), mentions the
occurrence of this genus in Texas.

Planocaprina trape^oides Palmer 1928.
?1898 (Caprina cf. adversa) Boehm, G. — Z. D. g. G., 50, pp. 326, 327 •
textff. 2, 3.

?1899 (Caprina cf. adversa) Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal.
Rep. Mexico, 2, pp. 147, 148; textff. 15, 16 (same text and figs,
as in 1898).

1928 (Planocaprina trape-n^pides) Palmer, R. H. — Occ. Pap. Calif Ac. Sc
14, pp. 65—68 ; textff. 7, 8.
(Burckhardt, p. 208).
Age : „Cenomanianquot; (Palmer, p. 24).
Loc. : Soyadan de Adentro, Jalisco, Alexico.

As has been seen on pp. 130, 131, Palmer considers the Caprina
cf. adversa rightly to belong to the genus Planocaprina. It may be identic
with Palmer's species.

Textfig. 7 of Palmer is wrongly orientated. So (near G) must be
changed into h\ and into Dp. The term is used by Palmer for two
essentially different things, viz. for the myophorous lamina of the right
valve, and for the septum of the left, which is confusing. On p. 65 Palmer
remarks that „The outer ends of the radial plates thicken until the edges
touch and then anchylose, forming what may be termed for convenience
the outer layer of the shell, which is very thin. As the term outer layer
is usually applied for a layer of different material and structure, which
seems to be absent here, this seems to me to be more confusing, than
convenient.

1922 Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer., 1 n. 135-
PI. 26, ff 1, 2.nbsp;' ' 1 »

Age : with Caprina pltwiensis and Amphiiricoelus.
Loc. : near the Plum Road, Eastern Trinidad.

The exterior likeness to Praecaprina is tlic base for the generic identific-
ation. I have failed to observe this similarity, as Praecaprina has the left
valve nearly symmetrically curvcd, whereas the West-Indian species is
most asymmetrically involute.

Praecaprina (?) pennyi Harris amp; Hodson.
1922 Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer., 1, p. 135 •
PI. 27, 3 ff ; 28, 2 ff

Sabinia kMgleri Bouwman.
1937 Bouwman, L. — Proc. K. Ak, Wet. Amsterdam, (in press).
Age: „? Senonianquot;.
Loc. : Point-a-Pierre, Trinidad.

Sabinia orbiculata Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 72, 73 ; PI. 13
ff. 2, 3.

The Caprinid nature of the ligament and the canal-pattern make it
probable, that the species indeed belongs to that subfamily, possibly in
the same genus as Sabinia kugleri. In accordance with this is the tabulation
of the canals. Of the lower valve no secdon is figured, which is highly to
be regretted in view of the discussion on pp. 144, 145.

Radial marginal canals in both valves; their walls bifurcadng? On
Palmer's PI. 13, f 3, the posterior tooth must be tought to be situated
more towards the antedor side, than is indicated by Palmer; not di-
rectly centrad of the ligament.

Sabinia totiseptata Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 73, 74 ; PI. 14, f 5.
1937 Bouwman, L. — Proc. K. Ak. Wet. Amsterdam, (in press).
(Burckhardt, p. 206).
Age: „Cenomanianquot; (Palmer, p. 24).
Loc. : Paso del Rio, Colima, Mexico.

Canals tabulated. Denddon and ligament unknown. Description and
figure insufficient. Generic posidon uncertain. No marginal canals!

Sabinia vivari Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, p. 74 ; PI. 13, f 4 •
14, ff. 1-4.

Dentition not preserved. Canals tabulated. Apparently no radially
stretched marginal canals. Marginal canals polygonal, not tabulated. In
Pl. 14 f. 3 a double ligament is figured, one an infolding into the inner
(„middlequot;) shell-layer, Caprinid-like, and another, forming a spur into the
visceral cavity. It is probable, that either the spur or the infolding has
nothing to do with the ligament. Otherwise the fossil would represent an
entirely new type of Rudist. The animal has much in common superficially
with the forms of the second type of evoludon, but the body cavity is not
tabulated. We cannot be sure about the systematical position of this fossil
but It is almost certainly not a Sahinia.

1936 Thiadens, A. A. — Proc. K. Ak. Wet. Amsterdam, 39, 9 pp 1140
1141 ; textf 5 (1).nbsp;' ' ^^ quot; '

Loc. : Southern Santa Clara, Cuba (loc. L 328, E of Matagua, cf Thiadens
textfig. 1).nbsp;onbsp;,

Canals tabulated. Ligament and right valve unknown, so that the
generic position is not certain (Thiadens, p. 1141). This species seems also
to occur at loc. M846 in Camaguey Province, Cuba, but the samples are
Ill-preserved, and gave no further palaeontological evidence (cf p. 9).

It is possible, that this genus does not occur at all in America cf pn
145, 150.nbsp;' ' ^^

About the difference of this genus with Coalcomana cf p. 148 note 16)
Its occurence in America is altogether doubtful.nbsp;'

Schiosia ramosa (Boehm) 1898, vide: Coalcomana ramosa.
Schiosia? in Palmer 1928.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 69 70
Age: „Maltrata-limestonequot; (Vraconnian = Upper Albian, 'in Burck-
hardt, p. 198).
Loc.: Orizaba, Vera Cruz, Mexico.

JV/./W^ .;, in Felix 1899, probably = Caprina sp. of Boehm, vide
Caprina sp. and ? Caprinuloidea sp.

1899nbsp;Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico 2 pp
148, 149; textf. 19 (same text and fig. as in 1898).nbsp;'

1928 (Coalcomana? or Caprinuloidea?) Palmer, R. H. — Occ Pap Calif
Ac. Sc., 14, pp. 61, 62.nbsp;'nbsp;' '

No right valve known. According to Palmer, it might be a Coalcofiiana
(p. 62), or a Caprinuloidea (cf. multitubijera) (p. 61). Coalcomana, however
must be excluded because of the numerous polygonal canals; probably it is
a lapsus for Caprinuloidea.

The specific difference with „Sph. occidentalis'quot; given by the author
falls away because of the wrong orientation of occidentalis, which has been
seen on p. 132 to represent a right valve instead of a left one. Its septum
is not a septum. Seen like this, the marginal canal-walls in the neighbourhood
of the real septum of the left valve, the position of which may be guessed,
appear to be unbranched just as they are in Sph. felixi.

The species may belong to the genus Caprinuloidea, in the neighbourhood
of C. ?7iultitubijera. Vide ?Caprifiuloidea felixi.

1899nbsp;Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico, 2, p. 149;
textf 20 (same text and fig. as in 1898).

Right valve and ligament unknown. The canal-pattern looks like that
of a Mitrocaprina (cf PI. 7, f 9). On the other hand the animal might
well belong to Caprinuloidea, which would be more compatible with the age
of the fauna. Its genus cannot be fixed with certainty. Vide ^Caprinuloidea
lenki.

Sphaerucaprina occidentalis (Conrad) 1855, in Boehm, vide Caprinuloidea
whitei (Boehm) (cf also Caprina occidentalis Conrad).

Sphaerucaprina sp. in Boehm.
1-898 Boehm, G. — Z. D. g.'G., 50, p. 330; textf. 8.
1899 Boehm, G. — Felix amp; Lenk, Beitr. Geol. Pal. Rep. Mexico, 2, p. 149;

Age: „Cenomanianquot; (cf. Palmer, 1928, Occ. Pap. Calif Ac, Sc., 14, pp.
24seq.).

Ligament and right valve unknown. Many polygonal canals. Generic
position uncertain. The animal might be a Caprinuloidea related to multi-
tubifera.

Lis «^rn Ifr^^^f^Sc'Sgc^^L '' quot;quot;nbsp;'nbsp;characteristic shape of 4. and presence'of marginal c^ands^tside

IÏtj 'r*'^!quot;'/'''. Paquier, V, 1905. Mém. S. g. F.; 13, 4 (Mém. 29), PI. 12, f. 2.
llld: Ofjnena rbodantca Paq. After Paquier, 1. c., PI. 12, f. 7.

ine: Caprinula oUsiponmsis Choff. After DouviixÉ, H., 1888, B. S.g.F., (3) 16, PI. 23 f 7b
Illf: Sabmia suhlacensis Par. After Parona, C. P., 1908, Bol. S.g.It., 27 textf b '
2: Paelytraga group Lpparenti Paq. After Paquier, 1. c., PI. 10, f. 5.
21: Praecaprina gaudryi Paq. After Paquier, I.e., PI. 11. f. 4.

2nc : ,Mitr0capri,u, (?) pl^cnsii' Par. After Parona, C. P.. 1908, Atti R. Acc. Lincei, (5), Mem. 7, textf. 25

2ne : SpbaerucapnnaaoodaardiGcmm. After D0UVIIJ.É, H., 1910, Mém. S. g. P., 18 Mém 41 textf 31

Innbsp;uaringi^Tiis amp; Hodson. After Harris, G. D. amp; Hodson, P.'. 1922, Pdeontógr.' Amer., 1. pl. 4 f 6

dllc : Coalfomana ramosa (Boehm). After Douvillé, H., 1900, B. S. g. P., (3) 28, textf. 3.nbsp;gt; gt; gt;

Slid : Caprinuloidea bisulcata Palm. After Palmer, R. H., 1928, Occ. Pap. Calif. Ac. 14 Pl 12 f 2

3IIc : Caprinuloidea whitei (Boehm). After Boehm, G.. 1898, Z. D. g. G., 50 textf l' ' ' '

3nf: Sabinia kugUri Bouwman. After Bol-wman, L. A. H., 1937, Proc. K. Ak. Wet.'Amsterdam, (in press)

From the aforegoing check-list results, that the only Caprinid genera
known with certainty to exist in the New-World are : Amphitricoelus, Plano-
caprina, Coalcomana, Caprinuloidea and Sahinia (kugleri !). The occurrence of
Caprina, Caprinula, Praecaprina, Schiosia, Sphaerucaprina is very doubtful, while
Kipia is an enigmatical genus of uncertain position.

Now the important point is, that the four first named genera have a
feature in common, that has never been observed in a single European
species This fundamental difference is bound up with the shape of the
cavity outside the right valve's posterior myophore. In the American species
this omp is always wide and comparatively short, connected with the pos-
terior alveole, but not with the ligamental cavity The section of this
Piv' omp cavity is more or less shaped like an ant's larva, or better, like
the ornament one often encounters on oriental tapestry. This cavity is
never subdivided quot;'), and set off sharply against the zone of peripheral canals
alongside it, which is never absent. The two alveoles are large, especially
the anterior one An', and the single tooth of the right valve 3 is situated
rather far from the circumference. Both valves have a distinct canal-pattern,
that of the right valve almost exactly copying that of the left. The latter
feature, although not as distinctive as the cardinal ones, is at least uncommon
in European forms (for instance Caprinula), and enhances the uniformity
between the American genera.

In the Old-World forms, on the other hand, the omp of the right valve
is long-drawn and narrow and distinctly separated from the Piv'- Its secdon
is longish, somedmes a litde curved parallel to the circumference. In the
European genera, canals may also be present in the right valve, (especially
outside the ?}ia but with the exception of Offneria, Caprinula and Sahinia,
not on the same scale as in the left valve, and on a different pattern. In such
forms, as do have peripheral canals outside the omp, this cavity is found
to be subdivided by radial walls and the large omp canals, formed by
this means are not set off sharply against the peripheral canals, which wedge
themselves often in between the omp canals with one corner. In other words,
a subdivisional wall between two omp canals, bifurcates, and the two branches

Except, maybe, by Wiontzek, H., 1933, Palaeontographica, 80 A, p. 32: „Ein Querschnitt einer
Unterklappe hat grosse Aehnlichkeit mit den von Palmer (1928) abgebildeten Caprimiloidea-hncn. Die
Bestimmung der Spezies ist jedoch nicht möglich.quot; Locality unknown I

«) In Sellaea where the omp is likewise connected with the Pi v' it is connected also with the ligamental
cavity, or at least extended beyond the ligament.

At the utmost one subdivisional wall has been indicated between the Piv' and the omp, cf. Palmer,
R. H., 1928. Occ. Pap. Calif. Ac. Sc., 14. PI. 12. f. 2. for Caprinuloidea bisulcata.

®) Canals outside the ma in the right valve, may already be present in a small way in Praecaprina (Pa-
quier. v.. 1905, Mém. S. g. F., 13. 4. Mém. 29. PI. 19, ff. 5. G) and Pachytraga (id.. PI. 18. f. 2).
They CKcur even in Sellaea. In the allies of Caprina there is often one row of them, for insunce in „Mitrocaprina
plmensisquot;. They are of little systematical value, as they may be present or not in one species, as in Caprina
schiosensis.

') If the muscle attachment is to be of the true Caprinid type, then the partitions cannot have rcachcd
up to the same height as the myophorous lamina itself, as otherwise, there would be no room for the myo-
phorous lamina of the left valve.

thus formed embrace the innermost corner of one of the larger peripheral
canals. In Offmria it is doubtful, whether there are peripheral canals at all
outside the omp, but the omp is much subdivided. In most forms there are
no regular peripheral canals in the right valve. Then the omp may be
subdivided i»), or undivided, or only subdivided at the bottom. The two
alveoles are small and submarginal, and so is the tooth Z.

This fundamental difference was first hit upon by Harris and Hodson
(1922, Palaeontogr. Amer., l,pp. 129, 130), who had it rather inadequately
worded. They call the American right valves „tripardtequot; as distinguished
from the others, that are „without a parddonquot;. It is clear, that the same
cavities occur in all genera, but in the American forms, where they are so
much larger, they impress themselves more upon the eye.

The distinction seems not to hold for the more primidve forms ^i), such
as Ethra and Sellaea, which look rather like the American type, and so
care must be taken to apply it only to such forms as have reached a certain
development. It is clear, though, that this was but to be expected, for, when
two groups develop from similar ancestors, their earlier stages, of course,
cannot be expected to differ as clearly as the more advanced ones.

We have not yet considered Sahinia, the only genus which seems to
occur in both parts of the world. Now it is most curious, that in Sahinia
higleri the same type oiPjv' omp cavity is found, as in the other American
Capnnids, though much reduced, whereas in S. aniensis from Italy the omp
seems to be endrely absent. Its posterior tooth alveole is simply rounded in
section, and not at all extended. And further still, the teeth are submarginal
in aniensis, whilst more internal in kugleri. So kjigleri corresponds to the
American type, whereas aniensis is more like a European Caprinid.

On these principles S. kugleri seems to be untenaljle as a Sahinia, and
it looks as if it were necessary to create a new generic name for it. I have
refrained from doing this on the following grounds: of a considerable
number of forms belonging to this subfamily the right valve is not known
at all, while in other cases it is insufficiently described. So the above disdnc-
tion is, as yet, in a rather theoretical stage, and has still to be tested in many
an instance before it will be definitely established. In this state of affairs
I am not prepared to introduce yet another generic name. When the distinc-
tion will have been proved to hold rigorously, then will be the time to
separate kugleri from the genus in which it is now provisorily retained.

Much confusion reigns in the further classificadon of Caprinids, which
is not to be marvelled at, seeing how the general principles of classification
had not been universally recognized, with the result that so many genera
of entirely different subfamilies had been mixed up with them. Now that
ihQ Plagioptjcbinae and the forms of the second type of inverse evolution have

The subdividing of this cavity occurs already in Pacbjtraga (cf. Paquier, V., 1905, Mém. 5. g. F.,
13,4, Mém. 29, PI. 18, f. 5) and also though very poorly in Praecaprina (Paquier, 1. c., Pl. 18, f. 11). (N.B. ncit
in Pl. 19, f. 2, for this figure represents a left valve, „mpquot; here is an error for ma).

quot;) In Ethra and Sellaea the ligament has not yet reached the development of the later Caprinids.

been removed from them, we may attempt to establish some order. To clear
the ground, the Old-World fauna must be considered first. We have to deal
with the foUowing genera 12): (Praecaprotina, Caprotina, Chaperia, Ethra,
Sellaea); Pachjtraga; Praecaprina; Caprina, Schiosia, Orthoptychus, Sphaeru-
caprina; Offneria, Caprinula; Sahinia (pp.). The first five must be dealt
with by someone more competent than I am. They offer so many problems,
that I must needs refrain from any further comment (cf. pp. 95, 100). They
form Douvillé's group of the Caprotininae. On p. 100, I have contended,
that it may be possible, that at least part of these forms had nothing to
do with the Caprininae at all, and that maybe they developed directly from
the Monopleurinae. In all Caprotine genera, the ligament has not reached the
same stage of development as in the Caprininae.

Pachjtraga has a cavity or canals outside the ma of the left valve. In
Praecaprina the canals are found outside the mp also, but they are still lacking
ventrally. In the left valves of all other genera canals are found from the
ligament down all along the ventral margin up to the region outside ma
Here sometimes true canals are found, sometimes more irregular hollows or
cavities of more indefinite shape. Offneria, Caprinula and Sahinia will be
treated on p. 149—151. The remaining all conform to a definite type, that of
Caprina, and may be considered more or less as subgenera of that genus. Much
confusion prevails here and especially the Schiosi Caprinids have given
rise to many a controversy. In the following will be given the author's opi-
nion of them, as acquired from the study of the literature only. The forms
concerned are strikingly alike in many respects and differ mainly in the
following points: the nature of the canals or cavities outside ma in the left
valve, and the general aspect of the canal-pattern of the same valve. Other
differences are merely specific or even variational. The nature of the oma
cavities or canals has been considered of first importance. Indeed it has been
pointed out by Douvillé i3), that in the Caprininae as distinguished from
the Plagioptjchinae, there are always large oma canals in the left valve. But
this is not true, as in practically all American genera and also in some of
the European forms true canals are found here, that do not differ much
from those found elsewhere on the circumference i^). Indeed Boehm dist-
inguishes Sphaerucaprina from Caprina just on account of the different shape
of the oma holes, very large and indefinite in Sphaerucaprina, rather regular
and comparatively smaller in Caprina. The shape of the oma cavities in
Orthoptjchus, for him, is additional proof of its identity with Sphaerucaprina.
The type of canal-pattern comes in the second place, for it marks an evol-
utional development only. This, without doubt, must be conceded, but,
on the other hand, the nature of the oma canals does not seem to be so
important either. First of all, as has been said above, there are many true

11} description of the genus Bicornttcopina (German translation) docs not make sense to me.

») In the Plagioptychime, moreover, outside the ma a long-drawn shallow depression may be developed
ct. p. Ibl, or even three distinct oma cavities, cf. p. 165.

Caprininae without any larger canals at all outside the ma, as for instance
in Sahinia and „Orthoptychus (?) striatusquot; (in Parona 1908), and then in
„Schiosia forojuliensisquot; (in Parona 1908) the oma are more or less intermediate
between the two types of Boehm. It is likely that the forms under discussion
belong closely together, and, as has been said above, that the different
genera deserve scarcely more than the rank of subgenera. So it is not very
important after all, what we take for a base in separating them, as long
as we realise its ultimate relativity. The canal-pattern proved itself to be
most tractable and admits of a much more speedy identification. In addition,
it allows us a better parallelization with other groups, which adds to clanfy
matters.

Six stages of specialization may be discerned in the canal-pattern of
Captinid Rudists, with peripheral canals ventrally.

c)nbsp;polyfurcated, giving rise to new sets of canals of second, third etc.
order. The larger canals are pyriform in section.

d)nbsp;tangential walls appear next, and polygonal canals are formed, few in
number at first, but steadily increasing in number with advancing evol-
ution. At first, the tangential walls extend littie influence upon the
general aspect, and the radial walls still dominate the structure, but
little by littie the tangential walls grow in number, becoming more in
the nature of anastomoses, until:

e)nbsp;the original set of radial walls can no longer be detected, except near
the margin. We have then a marginal row of radial canals, and inside
that a number of polygonal or rounded canals.

f)nbsp;at last, inside the marginal row of radial canals the entire structure is
made up of tier upon tier of polygonal or rounded canals. At first the
innermost canals are still the largest, but in the end the whole inner
shell layer inside the marginal row, consists of uniform and irregularly
distributed canals, which even invade the dental apparatus. The mar-
ginal canals have become very small.

These stages pass more or less into each other, or in a single animal
a certain stage is reached in one place, when the rest is still on a more
primitive level.

In the following table this principle has been applied for the arrange-
ment of a number of Alpine forms.

oma canals in the left valve, sometimes smaller, sometimes larger;
occasionally also in the right valve

*) Marks genera of which the right valve Is sufficiently well known, to ascertain the nature of the
right valve's omp cavity.

irregular and large ofna cavity in the left valve; right valve insu fficiently
known, reputed to have a canal-pattern comparable to that of the
left valve

„S. schiosensisquot; i®).
canal-walls polyfurcating posteriorly, only more so
oma canals in the left and right valve

canals outside the ma of the left valve, not larger and similar to those
elsewhere on the circumference ; right valve unknown

„Orth. (?) striatusquot; i»).
(c) canal-walls much polyfurcated, ventrally too, no tangential walls
said to be a left valve. Only the ventral side known

„Orth. striatusquot; i»).
walls polyfurcating (posteriorly and anteriorly) with a few tangential
walls posteriorly

irregular and large cavides outside the ma in the left valve; right
valve insufficiently known

quot;) Schiosia has been provisionally included, in spite of the author's assertion, that its right valve is per-
vaded by a similar set of canals as the left valve (by force of this, it was considered by him as a section
of Caprinula). Before a good section of the right valve is given, one cannot judge the truth of this.

quot;) „Schiosia schiosensis Boehmquot; in Parona, C. F., 1908, Atti R. Acc. Lincei, (5) 7, pp. 340—342; texiff.
27, 28. Boehm's original description ascribes „radiale Mantelkanälequot; to the genus Schiosia. This has been
taken too literally by Harris and Hodson (1922, Palaeontogr. Amer., 1, pp. 132, 133), and so they separa-
ted Coalcomana with polyfurcated canal-walls from Schiosia with radial canal-walls. Boehm's term, however,
applies also to polyfurcated walls, viz. : Z. D. g. G., 50, 1898, p. 324 (p. 145 in 1899, Felix amp; Lenk, Beitr.
Geol. Pal. Rep. Mexico, 2): ,,Er besitzt innere, polygonale und äussere radiale Mantelrandkanäle. Letztere
zeigen am Schlossrande Verzweigungen dagegen sind sie am Hinter- und Unterrande einfach, ungegabclt.quot;
All the same, as was pointed out by Harris and Hodson, on the original figure of Schiosia, no polyfurcated
walls are indicated, but then the fossil was badly preserved at the posterior side. The nature of the omp
in the right valve would give a much better base for a distinction of the two genera, but then wc do not
know anything about it in Schiosia. All the same we may tentatively assume that it will hold. Should this
be true, than one would be free, to ascribe to Schiosia also forms with, locally, polyfurcating canal-walls,
but with „European ompquot;. On the whole, the Schiosia schiosensis of Parona, is very similar to Boehm's
species and there is no reason not to agree with the generic determination of Parona. See also underquot;).

quot;) „Mitrocaprina (?) plavensis n. f.quot; (in Parona, 1. c., pp. 335—340; textff. 20, 21 ab, 22—20) cannot
belong to that genus, for it has an internal ligament, and is a true Caprinid. The canal-pattern, moreover,
is different. No other generic name is given to it here, because it is not certain, whether it could not be in-
cluded in the genus Schiosia. Aluch work must still be done, before we even start to know, where a genus
of this particular group ends and where begins. In this state of affairs it would be confusing to include it in
Schiosia and criminal to invent a new name for it.

quot;) „Orthoptychus (?) striatusquot; in Parona, C. P., 1908, Mem. R. Acc. Sc. Torino, (2) 59, pp. 155, 156;
textf. 12. At the ventral side the somewhat thicker place may be noted, where the septum has broken off.

quot;) „Orthoptychus striatus Puttererquot; in Wiontzek, H., 1933, Palaeontographica, 80A, p. 31; textf. 21.
Of this form, the ligament is not known, so it might as well, for ail wc know, belong to the Plagioptychinae.

'quot;) The type specimen, as figured by Boehm. Orthoptychus, it seems to me, need not be suppressed as
summarily, as has been done by Boehm. Genera have been established on less ground. It may be reserved
for those forms, which have polyfurcated canal-walls in the left valve, and with but a few, if any, tangential
walls (posteriorly).

o;m canals of the left valve large, but comparatively regular; right
valve unknownnbsp;„—forojuliensisquot;^^),

oma cavities in the left valve large and irregular; no regular oma
canals in the right valvenbsp;Sphaerucaprina.

being a mere extension of the omp and oma canals, of the 0. interrubta
group 22).nbsp;^

In Caprinula the canals appear to have differentiated into a set of very
large omp canals, separated by radial walls, and a row of marginal canals,
extending from outside the ma, along the ventral side, and thence continued
outside the omp canals. That part of this row, which is outside the ma
conforms to the oma canals of Offneria, so the oma canals belong to the
peripheral canals I It is probable that this canal-pattern is not fundamentally
different from that of Offneria, but that it arose from the latter by a process
of differentiation. This is the more probable, as the two kinds are not
sharply separated everywhere (viz. at the tip of the myophoral cavity).
The presence or absence of marginal canals outside the omp furnishes a good
generic difference between the two genera. In the left valve of Caprinula
outside the ma some large canals occur, of the same kind as those elsewhere
on the circumfercnce, but larger.

Summarizing, we find in the European Caprininae, with canals all
around the ventral side, two lines of development, both starting from
Praecaprina (Paquier, 1. c., pp. 82, 92, 93). In the main branch the further
development can be followed almost step for step. The forms differentiate
merely by the increasing complication of the canal-pattern in the left valves,

•') „Schiosia foroiulhnsis Hoclimquot; in Parona (1908, Atti R. Acc. Lincci, (5) 7, pp. 342 343- textf quot;gt;9)
AlthouRh his spccinicn h.is much more can.ils than the type specimen, Parona brought it'to this specfcs
bccausc the section figured by Bor.iim was cut at some distance from the commissure. I)(juviLLf (1888*
B. S. g. F., (3) I(), p. 720), however, has observed, that at least in the Plagiopt)chinat, the canals do not increase
in number with advancing age. But at a distance from the commissure the canals are often seen to have
been filled with limestone, which through recrgt;stallization may obscure the real nature of the structure
enormously. So it may be possible, that Bouiim's specimen had more canals, than one might think. Whatever
the ease, Parona's specimen cannot be reckoned to Schiosia, as its canal-pattern is incompatible with the
gcneric description of that genus. With regard to the canal-pattern, the spccics stands intermediate between
Orlbo[)ljchus and Sphatrucaprina\ with regard to the owa canals of the left valve, it stands apart

*') A good argument for this is furnished by OJlneria intermedia Paquier. Here the oma and ow/. canal-
zones reach already beyond the tips of the myophores (PAQt;iER, 1. c., Pl. 20, f. 2).

while the right valve remains virtually the same, sometimes developing canals
outside the ma, occasionnally also outside the mp, by the partitioning of
the omp cavity. The other line develops a regular canal-pattern in the right
valve also, first as an extension of the canals outside the muscle insertions,
but differentiated afterwards into marginal canals and omp canals.

The genus Sahinia stands by itself. Its species have been briefly reviewed
by Bouwman (1937, Proc. K. Ak. Wet. Amsterdam, in press).
We must first dicern between the American and the European forms. The
American species are: kugkri, orhiculata, totiseptata, vivari and sp. (in Thia-
dens). Totiseptata and vivari differ from the generic type through the lack
of radially stretched marginal canals; their generic position is not at all
clear, and vivari almost certainly does not belong to this genus. The American
species, with the exception of kugleri, are insufficiently known, and higleri,
as has been seen (p. 145) seems to belong to a different type of Caprininae,
than the European forms. The Mexican species have been referred to the
Cenomanian, without sufficient ground. A PSenonian age has tentatively
been suggested for the species kugleri. If our conclusions are right, this
species would be much more related to the Caprinuloideae, than to the
European Sahiniae. Caprinuloidea is referred to the Cenomanian by its author.
As has been seen on pp. 10—12, itis more probably of the same age as the Edwards
Limestone, i. e. of Albian age. Thus a Cenomanian age would be indicated
for the more evoluated Sahinia kugleri. The European species have been
referred to the Maestrichtian. As the type species occurs together with an
„Ichthjosarcolitesquot; there may be some doubt with regard to this (cf p. 53),
or otherwise with regard to the determination of the Ichthjosarcolites.
At Friaul the genus Sahinia is also reported from the Maestrichtian, associ-
ated with Orbitoids (cf. Klinghardt, 1921, Die Rudisten, 1, p. 61).
„Schiosia hilinguisquot; J. Boehm, from the Maestrichtian or Upper Camp-
anian (cf Kuhn, O., 1933, N. Jb. Min. etc., Beil. Bd. 70 B, pp. 229, 230)
of Bithynia, also may belong to this genus ; it is certainly not a Schiosia.
The „Sahinia klinghardtiquot; of the same author and from the same region
does not belong to the Caprininae, but is a Sauvagesia.

Now, as has been seen on p. 104, the Caprininae seem to have become
extinct after the Lower Turonian. So their reappearance in the Maestrichtian
would be improbable, though not impossible (cf p. 100, on the descendance
of Rousselia from Monopleurids). There are three ways, to account for
this difficulty : a) the Caprininae did not die out in the Turonian, but lived
on, up to the Maestrichtian ; h) the Sahiniae do not occur in the Maestrichtian.
This might be true for the type-locality, but the localities in Friaul seem
to form a different proposition; c) they do not belong to the Caprininae.
The type material, however, to judge from Parona's textf. a (1908, Boll.
Soc. geol. It., 27), presents all the characteristics of the Caprininae (ligament,
accessory cavity), with the exception of the omp cavity. It might yet be
a form developed from the second type of evolution convergent to the
Caprininae, but such an idea, without further proof, is rather far-fetched.

Through courtesy of Prof. F. Klinghardt and Prof. W. O. Dietrich, I could
examine some of the Friulan samples described by Klinghardt, but the
material was not sufficient to settle this question. Further material of this
genus must be examined with special attention to this problem.

If now we reconsider the American forms, we see, that the canal-
pattern of the right, valve is already distinctiy individualized from the first,
and on the same height of evolution as that of the left in the most primitive
form known, i. e. in Amphitricoelus, and this at a time when ventrally no
canals had developed as yet, and when none other than radial walls had
developed. There are even distinct marginal canals outside the omp, which
has its American nature already fully established. Afterv/ards we find an
almost continuous series of forms with canals all around the circumference
not only ventrally but also dorsally. Again they differentiate, as did the
European Caprininae, through the successive complication of the canal-
pattern. But here this differentiation takes place in the right valve too, hand
in hand with that of the left, the omp always retaining its characteristic kiape.
Once again the genera concerned may be considered as subgenera of one
genus. First in Planocaprina the walls occasionally bifurcate. They are poly-
furcated in Coalcomana, and traversed by tangential walls in Caprinuloidea 23).
The amount of tangential walls augments in the forms like C. multitubifera,
even as far as to obscure the original radial wall-structure (cf the Sphaeru-
caprina-stzgQ in Europe). In Sabinia ktigleri a uniform net of polygonal canals
with a marginal row of radial canals is developed. The omp Pjy' cavity
though still of characteristic shape is much reduced in this form. Sabinia
orbiculata seems to be intermediate between Caprinuloidea multitubifera and
Sabinia kugleri. But as no right valve is known of this species, we cannot
be sure about its position.

In the next chapter it will be seen, how the development in the Plagtop-
tychinae, though on a smaller scale, is strikingly parallel with that of the
different Caprinid branches. The following diagram illustrates this parallelism

Amphitricoelus

Planocaprina
\

Coalcomana
T

Caprinuloidea
\

Caprinuloidea
multitubifera etc.

Sabinia h)glen

quot;) Tangential walls arc already found outside the ma and in the posterio-vcntral comcr in Coalcomana.

It will be clear, that for the identification of Caprinids both valves
must be known. The right valve, to ascertain the line of evolution, the
left for the evolutional stage. Only in Offneria, Caprinula, Sahinia and in
the American genera an isolated right valve may suffice at the present
state of affairs. In all other cases an isolated valve cannot be identified.
An exact knowledge of the nature of the Hgament may also be indispensable.
The necessity of knowing both valves, already postulated by Douvillé and
Boehm, has become only the more necessary.

Because of the difficulty to define the Caprotininae from the Caprininae,
a check-list of the American forms of this group is given here, as a supple-
ment to the-list of Caprinids.

Baryconites multilineatus Palmer.
1928 Palmer, R. H. — Occ. Pap. Calif. Ac. Sc., 14, p. 52 ; Pl. 8, f 7.
(Burckhardt, p. 208).

Age: „Cenomanianquot; (cf Palmer and Burckhardt, p. 208).
Loc. : Soyatlan de Adentro, Jalisco, Mexico.

This genus and species has been put amongst the Caprotininae, although
the material is entirely insufficient to judge its systematical position. As
far as one can judge, the animal has a Monopleurid dentition, rather than
Caprotinid, with very thick shell-wall dorsally. It is not clear, why the
fragment has been named at all.

Caprotina hicornis Meek 1876 = „Requienia hicornisquot; (Meek).
Described by Meek under the name Caprotina (Requienia?) hicornis
Mentioned by Scott, G. (1926, thesis, Grenoble) and Adkins (1928, Texas
Univ. Bull. 2838) simply as Requienia hicornis.

Caprotina jerseyensis Weller.
*1907 Weller, S. — Geol. Surv. N. J., Pal. ser., 4, 5.

Caprotina senseni Conrad.
A full bibliography need not be given. It will suffice to quote Gabb,
W. M. (1862, Proc. Am. Philos. Soc., Philadelphia, 8, p. 240): „Mr. Conrad
has placed this species successively in Inocerawus, Arietina and Requieniaquot;.
Apparently the generic position is not quite certain.

Caprotina texana (Roemer) = „Toucasia texanaquot;.
Occurs in the literature as Caprina (?), Caprotina, Requienia and Toucasia.

A „Caprotina spquot; has been mentioned by Boese from the Escamela-
limestone (cf Burckhardt, p. 199). It would be necessary to consult
Weller's report, in order to know, whether the genus occurs in the New
World ; the occurrence of Caprotina in the Senonian, however, is improbable.
The other three species belong apparently to the normal series of Rudists,
or to an even different group.

Chaperia sodalis Palmer 1928.
1928 Palmer, R. H. — Occ. Pap. Calif Ac. Sc., 14, pp. 50, 51 ; PI. 8, f. 6.
Age : „Cenomanianquot;.

Description short. The animal lacks an external ligamental groove.
The generic determination does not seem sufficiently established.

Of the Polyconitinae a Horiopkura gregaria has been described by Palmer
(1928, Occ. Pap. Calif. Ac. Sc., 14, p. 49 ; PI. 8, ff. 1—5), from the „Ceno-
manianquot; of Paso del Rio, Colima, Mexico. Polyconites? has been mentioned
by the same author (1. c., pp. 52, 53) from San Juan Raya, Puebla, Mexico.
The age of the strata at this locality is Aptian or Barremian according to
Muellerried (1934, An. Inst. Biol. Mex., 5, 1, pp. 69, 70). Muellerried,
however, only mentions the occurrence of Himeraelites and Agriopkura at
this locality.

As contended on pp. 95—97, 104, this group cannot be reckoned to the
Caprotininae.

In contrast with the Caprininae, the Plagioptychinae are fundamentally
alike in the New World as in the Old. Some species have even been found
in both parts of the globe i).

This subfamily differs from the Caprininae in the following points: the
ligament exists as an inflection or a flexure of the outer shell-layer into the
inner one; it is not represented by an infolding that passes deep into the
inner shell-layer, forming a cavity at its end. Canals occur in the left valve
only, whereas the inner shell-layer of the right valve is structureless or
pseudoprismatic. In habitus they are characterized by the roundness of
their left valves and the near symmetry of the curvature of that valve.
Some other features are also mentioned in the literature that are not con-
clusive -) : a) absence of large oma canals or cavities in the left valve : they
may be also wanting in the Caprinids; b) absence of large omp cavities in

') Plag. amaudt Douv. and P. tourasiamu Math. (cf. Muellerried, F. K. G., 1933, An. Inst. Hiol.
Mcx., 4, no. 1, pp. 3—14). Also: Mitrocaprina hajani (Douv.), cf. p. IC4.

•) cf. Doiwillé, H., 1888, B. 5. r. F., (3) 16, pp. 724, 725; Douvillé, H., 1889, B. S. r. F.. (3) 17
pp. 646, 647; Boehm, G., 1895, Palacontographica, 41, pp. 102, 103, 109.

the right valve : there may be but one large o?np cavity in Caprinids, and
such a cavity is also developed in the Plagioptyclid Mitrocaprina ; c) paralle-
lism of the right valve's tnp to the commissure : this feature too fails to
hold for Mitrocaprina^).

The ofnp cavity is not present in the older forms, and appears only at
a later phylogenedcal stage 4), and so this group must have originated
independently of the group of the Caprininae, as a distinct but parallel
branch. Douvillé deems them direct descendants of Gyropleura^). They
belong to a new era, and only appear, when the Caprininae decline. On the
whole they seem to be younger than is commonly thought (cf. p. 27), and
it is questionable, whether they occur really in the Cenomanian at all®).

The simplest form known is Plagioptychus, with a recumbent t}ip lamina
in the right valve, a distinct ligamental groove on the exterior and
with a simple canal-pattern. The right valve may be low and gyrate or
conically straight. From this genus two genera descended independently.

In Mitrocaprina tangential walls develop and eventually the original
radial pattern is replaced by a network of polygonal canals, bounded out-
wardly by a marginal row of canals. The ligament is indicated by a mere
depression or flexure only of the outer shell-layer. The omp is well developed
in some of the species known to me. The right valve is low, exogyroid,
and largely adherent by the entire anterior half of its surface.

The genus Coralliochama was first referred to this group by Douvillé
in 1904 (B. S. g. F., (4) 4, p. 526). Boese points out its similarity in habitus
There is no doubt but that it is a true Plagioptychid : its ligament is marked
by an inflection of the outer shell-layer as in some species of Plagioptychus »),
but longer. This indicates that it was a direct descendant from Plagioptychus
and not from Mitrocaprina. The nature of the shell-structure points the

») also Ù1 Pîag. tibetkus Douvillé, 1916, Pal. Ind., (n. s.) 5, mem. 3, from the Maestrichtian of Thibet
cf. p- 16 : ,,du côté postérieur une lame myophore dressée venant se placer en dedans de la lame corres-
pondante de l'autre valve, disposition qui rappellerait celle que l'on observe dans les Caprinula.quot;

*) 1. c. in Mitrocaprina and in the Maestrichtian Plag. tibeticus (see the precedine note).

Douvillé, H., 1889, B. S. g. F., (3) 17, p. 647. In 1888, B. S. g. F., (3) 16, p. 725, he still regarded
the Monopleunnae as the direct ancestors.

•) Kutassy, Cat., mentions Plag. aguilloni d'Orb., cordatus Roemer, baueri (Teller) as occurring in the
Cenomanian. P. agutlloni, however, hails from the Upper Turonian of Southern France (cf. Douvii lé
Paquier Toucas in Haug, E., 1910, Traité de Géol., 2, 2, p. 1169. The alpine samples brought to thii
sixcics belong to the Upper Santonian-Lower Campanian, cf. Felix, J., 1908, Palaeontographica, 54, pp.
314,315; the Yougoslavian samples to the Campanian or Maestrichtian, cf. MiLovANovid Br 1932 Ann
géol. Pén. Balk., 11, 1, pp. 31, 71.nbsp;.....

The description of P. (?) cordatus does not make sense, but the animal ccrtainly does not belonc to
this genus.nbsp;®

P. haiuri, which undoubtedly belongs to this genus, occurs in the basal conglomerates of the cretaceous
near Teplitz, together with Radiolites bohemicus (Teller), an isolated fauna. They were referred to the Ccno-
manian by PoÇta Although I did not find it explicitly stated that these conglomerates belong to the
„leplitKr Schichten (Upper Turonian), it seems safe to assign this age to the species.
.loqn doubtful yj-a (only casts and moulds found) was mentioned by Zufpardi-Comerci, R.
(1930 Boll. R. Uff. geol. It., 55, art. 7, p. 9) from the Cenomanian, East of Poggiardo, Puglia, Italy.

') cf. also Parona, C. P., 1908, Atti R. Acc. Lincei, (5) 7, p. 319 : „Coralliochama White (ascritto
al gruppo del Plagioptychus).quot;

•) P. antillarum (Douv.), cf. Rutten, M. G., 1936, Journ. Pal., 10, no. 2, textfig. 4 j ; A arnaudi Douv.,
cf. Muellerried, F K G., 1933, An. Inst. Biol. Mex., 4, no. 1, p. 8. For the ligament oi Coralliod^ma
sec G. Boehm, 1895, Palaeontographica, 41, textfig. 7 and Pl. 11, f. 32.

same way : the presence of the tabulated canals in the right valve exacdy
as in the left proves, that this structure cannot represent the final stage
of complication of the Mitrocaprina network. It is a new kind of structure
into which the amorph inner shell-layer of a Plagioptychits was suddenly
converted 9). Seen in this light it becomes at once clear, why there are
pytiform marginal canals in the left valve only, and this in its turn con-
stitutes a retrospective argument for the appurtenance of the genus to the
group at hand. It may be surmised, that the similar structure of Antillo-
caprina, Titanosarcolites, Trechgt;?iannella and Rousselia was effected in the same
way, but here the origin of the structure is not so evident. Neither in
Coralliochama, nor in one of the other genera named, is there a sharp limit
between the pyriform or radial marginal canals and the „prismsquot;, but
neither is there between the pyriform canals and the amorph inner mass
of a Plagwptychus. Both belong to one layer and the „prismsquot; are not
essentially different from the marginal canals. So the name „tabulated canalsquot;
must be preferred to the term „prismsquot;. The different species of Antillo-
caprina show, that the presence of tabulae is not essential. Recapitulating:
Coralliochama h a Plagioptjchus with tabulated canals, where in the other
genus there is but an amorphous mass.

The undescribed genus Plesioptjchus Munier-Chalmas 1884 (in litt.,
nom. nud.)i®) belongs to this subfamily according to Astre. (1932, Bull!
Soc. Hist. nat. Toulouse, 64, 1, p. 65). Type species : Plesioptjchus lacvivieri
Mun.-Ch. 1884 (in litt., nom. nud.) from Ariege, Southern France.

For a summary of the New-Worid literature, vide Muellerried, 1933,
An. Inst. Biol. Mex., 4, 1, pp. 3—14.

The following names have been mentioned : P. antillarum (Douv.) 1927,
arnaudi Douv. 1888, (?) cordatus Roemer 1888,gt;wraj/j- (Whitfield) 1897^
toucasianus Math. 1842, tschoppi Palmer 1933. Moreover a PL sp. has been
mentioned by Trechmann 1924, and the genus is recorded from Texas
by Adkins 1930.

P. arnaudi and toucasianus, both Old-Worid species were rediscovered
by Muellerried in Chiapas (cf p. 153, note 1) n). P. (?) cordatus does not
belong to this genus (cf p. 154, note 6), neither does P. tschoppi, which is
a Mitrocaprina. P.jamaicensis is an assemblage of different forms, which may
belong as well to Plagioptjchus as to Mitrocaprina for all we know. The
descriptions are entirely insufficient. The same holds for the P. sp. of

') cf. also Muellerried, F. K. G., 1932, An. Inst. Biol. Mex., 3, no. 2, p. 178 and Klinghardt F
1922, Die Rudistcn, 2, p. 17.nbsp;' ''

'quot;) Pleshptjcbiu Municr Chalmas 1884, nom. nud., in litt. in Lacviviur, 1884, Terr. cr«St. dc I'AriiRc •
nom. nud. in Munier Chalmas, H., 1888, H. S. g. F., (3) 16, p. 819.nbsp;'

») Muellerried, F. K. G., 1933, An. Inst. Biol. Mex., 4, 1, pp. 3—14. One of these was apparently
referred to as „Phgioptycbus AnuiutU nov. var. cbiapasenstquot; by Muellerried in 1933, Gcol. Rundschau'
23a, Salomon-Calvi Festschrift p. 270.nbsp;'

Trechmann, For completeness sake, the descriptions of Whitfield and
Trechmann are given on pp. 166—168. The large specimen of Whitfield's
Pl. 15, ff. 1,2, upon wliich his small-type diagnosis is based, is evidently
to be considered the type specimen of the species.

The genus Plagioptjchus stands in great need of revision, whereby it
will be necessary to re-examine the endre material thus far described. In
the present state of affairs, a thorough examination of the Cuban material,
which for the greater part is badly preserved, would be as unnecessary as
it would be hopeless.

P. antillarum (Douvillé) 1927.
1927 (Coralliochama a.) Douvillé, H., B.S.g.F., (4) 27, pp. 53, 54 ;
textfig. 2.

1932 (nec Coralliochama) Muellerried, F. K. G., An. Inst. Biol. Mex., 3,
2, p. 178,

1936 (Plagioptjchus a.) Rutten, M, G,, Journ. Pal., 10, 2, pp. 140, 141 ;
textfigs. 4 c, d, f, j.

Muellerried showed, that this species cannot belong to Coralliochama.
Rutten regards the curious structure inside the marginal canal-zone as a
„Kalkmaschenquot;-structure. A re-examinadon of his material did but confirm
this view. It must be remarked though, that the marginal-canal pattern of
Rutten's material is less complicated, than that of Douvillé's figure 2.
Simple walls are fairly frequent. Otherwise the walls bifurcate once, seldom
twice, whereas in Douvillé's specimen double branching is very common,
while simple walls do not occur. As already explained above, it is impossible
to ascertain whether they should be separated specifically, and the best
policy is indeed to use the name antillarum for all these samples with „Kalk-
maschenquot; for the present.

Douvillé's specimen came from Arroyo Hondo, Camaguey Province,
Cuba; Rutten's material from Bernia (loc. L540: nos. N49, 30, 31),
San Juan de los Yeras (loc. H 196 : N 50, and 1935, Pal. 307) 12) and North
of Anton Diaz (loc. M557 : N 48) all in Northern Santa Clara i-quot;^), Cuba.

The samples N30, 31 and 1935, Pal. 307 were brought to the species,
the rest was not named specifically.

The left valve is elevated, the commissural angle about 145°. Right
valve conical, straight. Ligamental inflecdon disdnct. The animals lived
in groups.

Endrely comparable to Rutten's material is a left valve fragment
found S. of Verracos (loc. H 870 : W 66) Pinar del Rio Prov., Cubai»).
The pattern is just as simple. The interior is full of irregular „Kalkmaschenquot;.
A set of irregular cavities, differentiated from the „Kalkmaschenquot; to the
interior, occurs inside the canal-zone.

quot;) Refers to the Paleontological collection of the Min. Geol. Institute, of Utrecht.

For sketch-maps of these localities vide RinrEN, 1. c., fig. 1.
quot;) Vermunt. L. W, J., 1937, Journ. Pal. (in press).

Other samples from Pinar del Rio Prov., Cuba.
1937 Plagioptjchus sp.) Vermunt, L. W. J., Journ. Pal. (in press).

From the same locality as the last comes another fragment (W67),
with the canal-walls twice or thrice branching. The left valve is elevated!
The right valve shaped exactly as in Mitrocaprina.

Yet another left valve fragment (W 68), from San Diego de los Banos,
collected by Dr. Tschopp. Walls twice branching, left valve elevated.

Two flat left valves, externally very similar to the Mitrocaprina n. sp.
of p. 166. The canal-walls bifurcate once at the ventral side. At the anterior
side, one of these branches frequently bifurcates once more. At the posterior
a double branching is very common.

In one of the specimina there seems to be one polygonal canal at the
anterior side! This specimen has a shallow depression outside the ma.

The other has distinct siphonal depressions upon its surface, separated
one from the other by a slightly elevated interbande.

For a monograph of this genus see : Muellerried, F. K. G., 1932
An. Inst. Biol. Mex., 3, 2, pp. 169—179.

According to J. M. Muir (1936, Geology of the Tampico Region,
Mexico ; Am. Assoc. Petrol. Geol.), CoraUiochama g-boehmi Boese from the
neighbourhood of Cdrdenas, San Luis Potosi' (Muir, p. 72), and the CoraUio-
chama n. sp. of Muellerried (1931, An. Inst. Biol. Mex., 2, 2, pp. 175_i 77 •
textf 5), from Rayon, Tamaulipas (Muir, p. 74), both in Mexico, belong
to the Maestrichtian. The age of C. orcutti White is given by Kutassy (Foss.
Cat., 68, p. 166) as Senonian, by Muellerried (1932, 1. c., p. 175) as Lower
Senonian. It occurs in the Chico Formation. The age of the diverse parts
of this formation has not yet been definitely settled.

The following facts may be added to the previous descriptions. The
ligament is marked by a flexure and not by an inflection of the outer shell-
layer. Its course is parallel to the curvature and not to the commissure.
Outside the ma of the left valve one or more shallow depressions may be
present (PI. 7, fig. 5). The posterior muscle lamina of the right valve is
oblique (PI. 7, fig. 4), but erect, and separated from the margin by a distinct
omp cavity 1®). A horizontal section through the lower valve is exactly like

'») The internal nature of the right valve of M. bajani is not known. In M. ridali, the posterior recion
is not complete. The myophorous 1,-imina, however, is distinctly elevated in the neighbourhood of tooth 3
antl the area outside the muscle impression is distinctly depressed, as a shallow omp c.ivity, though ccrtainly
not on the same scale as in M. tscboppi.

that of a Sphaerucaprina but for the absence of a ligamental cavity. Indeed
it is one of the most astonishing facts in Rudist systematics, that Mitrocaprma
and Sphaerucaprina, so strikingly alike in many respects, should after all
belong to different groups, but there it is, undeniable.

European species : M. hayani (Douv.), type species, from the Lower
Campanian of Rennes-les-Bains (Aude), and possibly also from the Upper
Santonian of Ley chert (Ariège at Corbières) i®) both in France. This
species is also found in Cuba (vide p. 164). Further: M. vidali Douv.,
from the Maestrichtian of Pobla de Ségur, Lerida, Spain i').

The small specimina of „Plagioptychus paradoxusquot;, probably from
Mardgues, Bouches-du-Rhône, described by P. Mathéron (1842, Cat. méth.,
etc., p. 114) seem also to belong to this genus i®). Similar valves are of
frequent occurrence near Martigues according to Munier-Chalmas If
this is true, then the genus occurs also before the Campanian, for the
„régime saumâtrequot; of this region sets in with the Campanian.

Mitrocaprina tschoppi (Palmer). (Pl. 5, f. 7; 7, ff. 1, 4, 5, 7, 8; 8,
ff 4, 7).

1933 (Plagioptychus tschoppi) Palmer, R. H. — Rev. Agric. Habana, 14,
nos. 15, 16, pp. 103, 104 ; Pl. 10, ff. 1—3 (in the explanation of
Pl. 10, the heading of fig. 4 has been omitted. It represents the
„Coralliochama (i) sp. (i)quot; of p. 104).
1936 ( Caprinid fragment) Thiadens, A. — Proc. K. Ak. Wet. Amsterdam,

39, 8, p. 1011, line 9—12 ; textf. 3 (13).
(1937 (Mitrocaprina tschoppi) MacGillavry, H. J. in Thiadens, A. —
Geol. Geogr. Med., Utrecht, 12, p. 43.
Material: 9 specimens from the type locality, Ciego de Avila, Cama-
guey Prov., Cuba. (Nos. Ca 85—93). Most of these were found by Dr.
Tschopp ; the remaining were donated by Dr. Palmer.

Exterior: Large species, much larger than the two European species.
The largest specimen (Ca 85) (Pl. 7, f. 1) has a diameter of 98 (ant.-post.)
by d: 70 mm near the commissure. Its left valve measures about 190 mm
along the outer curve. It is exceptionally large, but samples with a diameter
of 80 mm (ant.-post.) are quite common. Inaequivalve ; left valve similar
to that of Coralliochama orcutti White, smooth, nicely rounded (Pl. 8, f. 7).

quot;) cf. Douvillé, H., 1904, B.S.g.F., (4) 4, p. 529.
quot;) cf. Douvillé, 1. c.

quot;) cf, Douvillé, H., 1888, B.S.g.F., (3) 16, p. 716.
») in Douvillé, le., pp. 715, 716.

The umbo less inflated and less saliant over the commissure than in M.
bajani Douvillé. It is almost symmetrically curved. The umbo is anterio-
dorsal, near the boundary between tooth 3 and An. So the dentidon is
a little asymmetrically arranged with regard to the curvature, i.e. the
curvature is a litde deplaced towards the anterior side. There is a scarcely
perceptible helical departure from symmetry of the curve in the younger
stages, which diminishes rapidly with advancing age of a specimen. It is
directed towards the posterior side. As a result the umbo is turned a littie
backward (Ca86, 88, 89) 20). It is not knowA, whether this is constant, as
Ca 90 gives the impression of having the umbo turned a littie forward ^i).

Outer shell-layer thin. Best preserved in Ca86, where it is 0,2 mm
thick at the ventral side (PI. 7, f. 5). Mostly preserved in patches only.
It becomes thicker towards the dorsal side, but is often thinner again,
where it comes into contact with the eariier stages of the shell 22).

The ligament is marked in the left valve by a rather sudden depression
or rather a flexure of the inner margin of the outer shell-layer. This depression
is at least partiy, if not entirely, filled with a thicker mass of outer-shell
layer, but visible nevertheless from the outside (PI. 7, f. 5). It follows
the curvature of the valve and so it is not parallel to the commissure, but
neariy perpendicular to it. The helical tendency of the curve has no'per-
ceptible effect upon its course, because of its nearness to the umbo. The
symmetry of the curvature is accentuated by this.

In the young specimen Ca 93 a lunula seems to be differentiated (cf.
Pl. 5, f 7), which, however, could not be retraced in the other samplesquot;
probably because of weathering.nbsp;'

Right valve entirely different. A littie, sometimes much smaller than
the left ; adhering with half its surface to foreign objects (cf Association).
This area extends itself over the entire anterior side, during the entire life
of the animal (PI. 8, f. 4). As a consequence the animal grows along
this plane. It is sharply distinguished from the other half of the surface
and separated from it by an angularity, ToncasiaA\k(^ 23). it ig smooth, polished,
and follows the substratum, whereas the posterior half is roughened by
growth layers and retains its own form (PI. 8, f. 4). It grows in a low
spire, parallel to the substratum at the anterior side, but away from it at
the posterior side. As a result, the commissure if seen from the ventral
side is inclined towards the substratum towards the anterio-ventral corner.

in the co lections of the Geol. Inst, of Amstcrd.im (cf. also Muellerried, 1932, An. InstT kol Mex
' '.iCquot; J • quot; ; ■ . 'nbsp;cnrollado hacia atrds,.. quot;).

quot;) Palmer (p. 104) remarks, that there is great variability. In my material, however, there is but
little variation in most respects.nbsp;, ». i.

This angularity may be so sharp, that one gets the impression, that the right valve is broken along
a fault-plane. W.ntfield may have Ikcii deceived by a similar disposition of the right v.ilvc in .,/W
ptjcbus jamauenm , viz.: „ .. having the basal portion of the lower valve broken awayquot; and acain- the
lower valve is crushed and comprcssedquot;. cf. also Douvillé (1888, H. S. g. F., (3) 16, p. 726 bàyani) •
„valve inférieure était courte, conique et tronquée h sa base par une large surface d'adhérencequot; a correctquot;
but deceptive description.nbsp;'nbsp;'

This valve often is very flat, so that in fixed specimens only a small stretch
of its outer surface is visible, depending upon the shape of the substra-
tum. The umbo is situated at the posterior side of the left valve and ante-
riorly directed (PI. 8, f. 4). Because of this position of the umbo, the
ligament of the right valve could not be found

The outer shell-layer is distinctly thicker than that of the left valve.
It may reach a thickness of 2 or 3 mm at the ventral side. Dorsally it is
thicker still. Its structure could be ascertained in Ca 85. It consists of
extremely thin, compact lamellae, of varying colour. But, as a whole, the
colour of the outer shell-layer is darker than that of the inner shell-layer.
The lamellae are steeply inclined towards the interior. It could not be
ascertained, whether they are parallel to the labrum. This, however is very
probable, and would agree with Palmer's (p. 104) description: „Lavalva
inferior forma un caliz bajo en el cual la comisura de la valva superior
entra.quot;

Internal features: The dentition is exactly like that of a Plagiop-
tjchus. The anterior tooth and muscle impression are separated from the
margin by a shallow depression (Ca86) (PI. 7, f 5). This depression has
nothing to do with the ligament. The two teeth must be short. Otherwise they
could not be straight because of the oblique growth of the right valve, and
could not be curved in a backward direction, because of the left valve's
nature. The truth of this could be ascertained for the Pjy of Ca 85. The
muscle lamina of the right valve is obliquely but strongly raised as a real
lamina, strongly inclined towards the exterior and separated from the margin

Fig. 1. Mitrocaprina tsciioppi (Palmer). Horizontal section through left valve of Ca 85, ventrally 16 mm
from commissure. At the top of the figure the umbonal stage with curious holes (? boring-holes). A
patch of the right valve's outer shell layer, with commissure, adheres to tooth 3.

Fig. 2. M. cf. bayani (Douvillé). Horizontal section through right valve of \V69, with the butts
of An and PiY. Plv' not differentiated from omp at this height.

Fig. 3. i\I. bajani (Douvillé), Horizontal section through right valve of \V70.

Fig. 4. M. tscboppi. Tangential section through the posterior region of Ca 87. The' most dorsal point
is reached near the middle (Piv). Above and below, the section falls off towards the ventral side owing
to the shell's curvature. The ventral part of the septum is just touched to the top right of the figure
The posterior muscle insertion of both left and right valve is well visible. Note the deep omp cavity and
the obliqueness of the muscle lamina in the right valve. Tooth 3 is joined by a lamina to the posterior
muscle lamina. The left valve s surface, just above the commissure is roughened by growth stages

Fig. 5. M. tscboppi. Horizontal scction through left valve (Ca86). Showing the ligamental depression
of the outer margin of the inner shell layer, both in the large and in the umbonal scction. Note the
depression outside the ma. At the posterior side, the shell's outline and the course of the ligament have
been projected into the figure.

Fig. 6. M. palmen n. sp. Type specimen. Horizontal scction through left valve, with Plai/iopty-
cous-hkc structure at the ventral side, and large tooth 3.nbsp;^ rj

Fig. 7. M. tscboppi. 1 lorizontal section through left valve of young specimen (Ca 93). The structure
is less complicated than in the large Ca85 (fig. 1), but only slightly so.

Fig. 8. M. tscboppi. Ca88. Subradial scction through right valve and commissure, showing the
anterior muscic insertion, lowness of right valve, and the angularity, which limits the area of attachment
(anterior side).

Fig. 9. M. bajatii. Horizontal scction through left valve of \V70. Showing simple canal-pattern
with large polygonal canals. Note pseudo-ligamental cavity in left top comer.

by a ptetty deep myophorous cavity. The muscle scar is well visible as a
thickening upon its external face (Pl. 7, f. 4). The omp cavity is not
separated from the posterior alveole. Both form one continuous cavity.
In accordance with this the muscle lamina passes without change into the
alveolar septum, becoming more and more raised above the commissural
plane until it joins the median tooth. In sections through the upper valve
it manifests itself as a sort of tail to this tooth. This arrangement is much
as in M. vidali DouviUé (1904, B. S. g. F., (4) 4, Pl. 13, f. 5), but there
the lamina is less erect, the myophorous cavity is much less impressed,
the posterior alveole is much deeper and differentiated from the myophorous
cavity. The section of tooth 3 is curved in accordance with the growth direc-
tion of the right valve, and so this tooth, in contrast with what we have seen
with regard to the two left valve teeth, can be large, and indeed is enormous.

Structure: There are about two rows of polygonal canals, and outside
these a row of radially stretched marginal canals. Their walls show occasional
bifurcations near the periphery. In the largest specimen (Ca 85) the marginal
.canals became enormously (but not disproportionately) stretched radially,
up to 10 mm, and here anastomoses halfway down their length are of
common occurrence (Pl. 7, f 1). The innermost half retains its radial charac-
ter and can be easily distinguished as such from the adjacent polygonal
canals. There are about 200 of these radial canals in the largest sample.
The increase in number with growth must be small, as in the smallest
specimen (Ca93, diam. 30 mm ant.-post.) there could be counted about
150 of them. This agrees with the scarcity of the wall-branchings, for these
bifurcations probably represent the intercalation of a new canal. The polyg-
onal canals too scarcely increase in number, and, in accordance with this,
they are almost all of comparable size. Barely any smaller canals, which
might be taken for intercalated new ones, can be found. The structure of
a small sample is almost as complicated as that of a large one. The diameter
of the canals increases in proportion with that of the shell itself (cf.
Pl. 7, ff. 1, 7). This concurs with Douvillé's observations onPlagioptjchus-'^).

The canals are not tabulated. Even in sections cut far from the com-
missure they may be filled with the same sedimentary material as the body
cavity. A certain amount of filling with calcite does occur, however, and
in these higher sections, the structure is obscured to some degree by the
recrystallization of it.

Outside Piv (Ca88), at the dorsal margin in the younger stages (Ca85,
Pl. 7, f. 1, top) and in the external margin of tooth 3 (Ca 88) some
irregular cavities are found that nevertheless conform to a certain type.
I am at a loss, whether they belong to the animal, or whether they arc
boring-holes made by some outside organism.

. Specific diagnosis: Very similar to M. vidali, but much larger.
Left valve like that of Coralliochama orcutti and thus intermediate between

that of M. bajani and vidali. Canal-system as in vidali. Teeth, especially the
posterior one short. Posterior myophorous cavity deep, and the/quot;/k'alveole
not differentiated from it. From bajani it differs by the much greater number
of canals.

Association: Ca92 grows upon the posterior side of Antillocaprina
annulata (Palmer) Ca 62, left valve (Pl. 8, f 7); Ca 93 upon the Pventral side
of A. annulata Ca56, right valve (Pl. 5, f. 7).

Observation: The second „Caprinid fragmentquot; of Thiadens copies
exactly the posterior side of Ca 89.1 have no doubt but that it belongs to this
species, and have cited it in the synonymy accordingly. There are some
unquestionable boring-holes in this fragment.

1933 (Coralliochama (i) sp. Palmer, R. H. — Rev. Agric. Habana, 14,
nos. 15, 16, p. 104 ; Pl. 10, f. 4 (on p. 104 of his text erroneously :
figs. 1-3).

Canal-walls bifurcating one to three times ; some polygonal canals
presentquot; There are about four polygonal canals in fig. 4, all situated
outside the posterior myophore. No data about the ligament.

In our collection is a right valve (Ca 95, Pl. 5, f 8), which un-
doubtedly belongs to a Plagioptjchus or Mitrocaprina, and which was found
at the same locality : V 529, Loma Yucatan. The omp is slightly impressed ;
exactly how much, it is not possible to ascertain, as the myophorous lamina
is pardy broken. A posterior alveole is not differendated as such. The
specimen is much smaller than Palmer's sample, only measuring 31 by 32 mm.

Observation: It is not proved, that the two valves belong to one
species and so it is not proved, that Palmer's animal belongs to the genus
Mitrocaprina.

Two specimens of a very curious type were found in Cuba by Dr.
Tschopp. To my regret the collector's number was lost here.

It differs from all other species by the aberrant canal-pattern of the
left valve. At the ventral side, the canals are exactly as in a Plagioptjchus:
pynform canals separated by walls, which bifurcate once or not. Towards
the septum, the structure becomes more complicated. First the walls bifurcate
twice, and then almost suddenly they anastomose and an intricate network
of rather irregularly distributed, often lanceolate canals is formed. There
are often four of them between the marginal canals and the body cavity.

species. This is illustrated by the great size of the umbo in the section figured.
There is a slight helical departure from symmetry towards the anterior side.

The commissural angle could not be measured, but it must be greater
than in M. tschoppi. The shape of the right valve could not be ascertained.
Tooth lt;3 is very large. There is a distinct ofnp cavity, and no Piv' alveole
could be found. The thickness of the outer shell layer of the left valve is
at least 2 mm, ventrally.

The largest, most complete sample (type specimen) measures 50 (ant.-
post.) by 34 mm. It measures about 100 mm along the outer curve. The
other has a section of 34 (ant.-post.) by 23 mm.

It was found together with Vaccinites inaequicostatus vermunti n. sbsp.
(cf pp. 118, 119) and a Nerineid.

Observation: the species seems to come nearest to the preceding
species, because of the limiting of the polygonal canals to the posterior side.

See Kutassy Cat., p. 158 for previous literature.
1937 (Sphaerucaprina sp.) Vermunt, L. W. J. — Journ. Pal. (in press).

ÎVlaterial: A specimen from loc. H 787 (^ km S. of San Diego de
los Banos, Pinar del Rio Prov., Cuba) (W 70). Another, very small and
young one from loc. T 835, collected by Dr. Tschopp (2,2 km N. of Con-
stancia, W. of Cienfuegos, Southern Santa Clara, Cuba).

The section of the largest specimen (\V70) is exactly the same size
as that of Douvillé's sample of PI. 25, f. 7 (nat. size, cf Douvillé's
text, p. 726). The canal-pattern too is almost exactly alike (PI. 7, f. 9).
The French sample shows a helical departure from symmetry towards the
anterior side, and so do the Cuban samples. The umbo of the left valve is
less inflated and less salient than in the French sample figured, but it is
distinctly more elevated than that of M. tschoppi. The canals are distinctly
greater than those of a M. tschoppi of about equal size (Ca 93). There is
one discontinuous row of polygonal canals with one or two times an additi-
onal polygonal canal (one or two near the septum, and one at the anterior
side). The row of polygonal canals is more continuous at the posterior side.

The cavities outside the ma described by Vermunt are inside the
canal-zone, and may be boring-holes. There is a similar hole at the very
place where a ligament might be, and this was taken for the ligamental
inflection by Vermunt. However, it does not bear the character of a liga-
mental cavity, and may also be thought to be a boring-hole (cf PI. 7, f 9).

Of the right valves littie could be discerned. \V 70 (PI. 7, f 3)
seems to have a distinct omp cavity, longitudinally stretched and, at this
height at least, not separated from the Piv' alveole. The internal features
of the European samples of M. bajani are not known.

Association: Both samples are imbedded in and filled with organic
suboolitic limestone with small Miliolids (W70). The young specimen
grows upon a small Biradiolites with denticulate structure ; this Biradiolites
is similar to those found upon the Antillocaprinae of Ciego de Avila.

Mitrocaprina cf. bajani Douvillé 1888. (Pl. 7, f 2).
1937 (Sphaerucaprina sp.) Vermunt, L. W. J. — Journ. Pal. (in press).

To the species bajani probably also belongs a bivalve specimen from
loc. V 614 (2,5 km W. of San Juan y Martinez, Pinar del Rio Prov., Cuba)
(W 69). The right valve is well preserved, and shows the situation of the
teeth. At this height the Pjv' alveole is not separated from the omp cavity.
The Piv tooth is comparatively longer than in M. tschoppi. The omp cavity
is well developed (fig.). Its diameter is 43 (ant.-post.) by 30 mm, its
total height about 25 mm. The left valve is rather flat.

Mitrocaprina sp. indet.
1937 (Caprinid fragment) Vermunt, L. W. J. — Journ. Pal. (in press).

From the loc. H 774 (5 km NNW. of San Juan y Martinez, Pinar
del Rio Prov., Cuba) (W55a) hails a small specimen with much elevated
left valve. Its diameter is about 35 mm. It has an intricate and rather irregular
canal-pattern, more complicated than that of M. tschoppi. The right valve
is incomplete and no section could be cut through it. From the M. n. sp.
from Catadupa (p. 166), which it resembles on account of the intricate
pattern, it differs by the elevation of the left valve.

It is grown upon by the Bournonia sp. described by Vermunt (1937
1. c., textfigs. 2d, 3k ; PI. 37, ff 4, 5).

An isolated left valve from loc. H 774 (5 km NNW. of San Juan y
Martinez, Pinar del Rio Province, Cuba). Its elevation is a little less than
that of M. tschoppi. Section about 30 (ant.-post.) by 21 mm. The dentition
partly freed by erosion. There are three distinct cavities outside the ma,
the cavity nearest to the tooth being the largest.

The canal-pattern is more complicate than that of bajani. There is
about one interrupted row of polygonal canals, about the same size as those
of that species. There are more peripheral canals, however, than in bt^'ani
and less than in M. tschoppi. Several peripheral canals are interrupted by a
tangential wall uniting the two radial walls. The radial walls are simple,
or they bifurcate once, and then one of the branches may bifurcate yet
another time.

A bivalve specimen from loc. H 698 (San José de los Jibaros (Ingenio
Grande), Camaguey Prov., Cuba) (Ca94). The ant.-post. diameter is a

little more than 30 mm. The left valve is very flat, whereas the right one
is comparatively high. It resembles the specimen of „Caprina jamaicensis'''
of Whitfield's Pl. 13, ff. 1, 2. The umbo of the right valve overgrips
the commissural plane. The polygonal canals are similar in size to those
of M. hayani, but the peripheral canals are smaller and more numerous than
in that species, about as numerous as in tschoppi. At the posterior side the
polygonal canals are more numerous, about three in a radial direction, oval,
irregularly distributed. Likewise in the region of the septum they are oval,
irregularly distributed, about two in a radial direction. This species may
be identical with the next. It is distinguished from those described above
by the canal-pattern and by the flatness of the left valve.

The collection of the Basel Museum contains a small left valve from
Catadupa, Jamaica, which belongs to this genus. The diameter is 30 (ant.-
post.) by 20 mm. It is distinguished by the canal-pattern, which is still
more complicated than that of M. vidali and tschoppi. At the posterior side
and in the anterio-ventral corner, there are at least three zones of polygonal
to oval canals. These canals are irregularly placed and not even disposed
in an approximation of rows. At the ventral side the structure is oblitera-
ted. Here the canals seem to be somewhat more regular and less in number,
more arranged in about two rows.

The flatness of the left valve separates it from Mitrocaprina sp. indet.
(W 55a) ; the intricate canal-pattern from all other species.

From Jamaica a whole series of forms has been described by Whitfield
and Trechmann, that belong either to Mitrocaprina or to Plagioptychus.

As species of Plagioptychus and Mitrocaprina occur together at the same
locality in Jamaica (cf. p. 157), the left valves of which cannot be distinguished
from one another from the outside, there is no means to tell, whether the
species described there, belong to one or the other of the genera concerned.
In the absence of precise data on the canal-pattern, we cannot even
trie to judge their position among the forms described above.

Abstracts of Whitfield's and Trechmann's descriptions are given
here, for comparison.

Mitrocaprina or Plagioptychus jamaicensis (Whitfield).
1897 (Caprina jamaicensis) Whitfield, R. P. — Bull. Am. Mus. Nat. Hist.,
9, p. 192, line 7—19 ; Pl. 15, ff. 1,2.

„Shell large and ponderous, having a diameter across the top of the
lower valve of eight inches. Lower valve very oblique, broadly spreading
and very much curved, shortest on the hinge side ; its substance quite

thick and strongly marked by irregular concentric ridges or growth lines.
Upper valve thin, smooth or with microscopic lines on the exterior; beak
large, incurved and overhanging the cardinal side of the lower valve.
Within, the shell of this valve is marked by fine, thread-like grooves radia-
ting from the apex.....having the basal pordon of the lower valve

broken away and one endre side crushed in so as to nearly destroy the
original contour.quot;

This enormous species would belong to the \a group, if it appears to be a
Mitrocaprina. It differs from M. tschoppi and palmeri by the left valve, which
is less elevated, the commissural angle being about 115° instead of the 140°
of tschoppi and the still greater angle of palmeri. From the Yucatan species
it cannot be distinguished on account of our insufficient knowledge of both.

Mitrocaprina or Plagioptychus sp.
1897 (Caprina jamaicensis) Whitfield, R. P. — Bull. Am. Mus. Nat.

„A small shell, having its broadest diameter one and three-fourth
inches, is oval in outline on the upper valve, with the apex of that valve
only slightly enrolled ; . . lower valve crushed and compressed so as to
obscure the original form.quot; If the figures really belong to this specimen and
not to the next, it would belong to group II, if a Mitrocaprina at all.

Mitrocaprina or Plagioptychus sp.
1897 (Caprina jamaicensis) Whitfield, R. P. — Bull. Am. Mus. Nat. Hist.,

„A second upper valve of nearly the same size as the last, has the same
general form and character, being thin and semitranslucent, with the radi-
ating lines of the interior showing through its substance.quot;

Mitrocaprina or Plagioptjchus sp.
1924 (Plagioptjchus jamaicensis) Trechmann, C. T. — Geol. Mag., 61,

„This fossil has all the essential structure of a Plagioptjchus ; the interior
of a top valve I developed shows a pointed anterior cardinal tooth supporting
a septum which projects down into the visceral cavity ; a socket for the
opposing tooth, and an elongated posterior tooth with behind it three
marginal accessory cavities, whose use is uncertain ^o). All my specimens
are small, up to 55 mm across the valves, and are closely attached by the
anterior side of the right valve ... It occurs at Logie Green ; in the Great
River Valley, and elsewhere.quot; Jamaica. The mendon of three accessory
cavity is the most striking item of this description. It is not clear, what

quot;) It is dear from TRirnMANN's description, that these cavities are indeed to be found behind the
posterior myophore, and not, as in the Mitrocaprina sp. of p. 165, outside the anterior myophore.

kind of cavities these are. They would be very much out of place in either
a Mitrocaprina or a Plagioptjchus.

Mitrocaprina or Plagioptjchus sp.
1924 (Plagioptjchus jamaicensis) Trechmann, C. T. — Geol. Mag., 61,
p. 408, line 5—8.

„The top valve of another species of Plagioptjchus occurred in the
Barrettia bed at Green Island; it is 80 mm long, 88 mm wide, and 54 mm
high, and has a rapidly tapering and rather anteriorly directed incurved
beak.quot;

If a Mitrocaprina, then it belongs to the \a group. It cannot be differ-
entiated from the species described there.

p. 29, line 35 : Amphistegina lope:(trigoi Palmer has been described from the
Lower Middle Eocene of Yecuatla, Veracruz, Mexico, by Barker, R.W.
amp; Grimsdale, T, f., 1936, Journ. Pal, 10, 4, p. 233. So it is possible,
that the Maraguan Sierra is partly or entirely older than Upper Eocene.

p. 61, line 29: add: DouvillI H., 1900, B.S.g.F., (3) 28, p. 230:
„Campanien supérieur (Maestrichtien ou Dordonien).quot;

p. 102, note 24: O. Kuhn, 1937, Zentr. bl. f Min., etc., B, 5, p. 237
comes to the same conclusion : „Wenn bei den Siphonalpfeilern physio-
logisch wichtige und dafür besonders geeignete Stellen vorgefaltet
wurden, so erhöht dies den Vorteil der ganzen Einrichtung, muss
sie aber nicht bedingen.quot;

Kipia triiiitaria Harris amp; Hodson 1922.
1922 Harris, G. D. amp; Hodson, F. — Palaeontogr. Amer., 1, pp. 133,

134; Pl. 24, ff 1—6.
Age: with Amphitricoelus iraringi. „Aptian, Albian or Cenomanian?quot;.
Loc.: Near the ö'/j mile post. Plum Road, Eastern part of Trinidad.

Material insufficient; description rather unintelligible. For instance
it is scarcely possible to ascertain, whether fig. 6 represents a left or
a right valve, the text as well as the explanation of plate being inconsistent
on this point. The left valve is said to have a cavity for the myophore
of the opposite valve. That would be most extraordinary.

Plate 8. Bournonia nov. sect. ; Antillocaprina; Antillocaprina aff. gen. B. ; Mitrocaprina.

Fig. 1. Antillocaprina annulata (Palmer). Anterior view of Ca 54, right valve with growth stages.
± X 1/2.

Fig. 2. Antillocaprina annulata. Posterior view of Ca3, with rather deep E groove, angularity for /,
and a slight flattening for the S zone. Note rapid tapering of the shell. ± X 3/4.

Fig. 4. Mitrocaprina tschoppi (Palmer). Bivalve specimen Ca90. Right valve with smooth anterior
area of attachment, exogyroid umbo, and the posterior face crossed by growth stages. To the top right
the umbonal parts of the left valve and below that the commissure. ± X 4/5.

Fig. 5. A. pugniformis (Palmer). Posterior view of bivalve, nearly aequivalve specimen (Ca65).
Showing deep siphonal depression. The section is figured on PI. 1, f. 5. ± X 3/4.

Fig. 6. A. crassitela n. sp. W 115.1, type specimen. Section through the right valve, showing
ligament, posterior tooth and anterior muscle area. For more detail see a drawing made from this
section (PI. 1, f. 9) and the detail figured on PI. 9, f 3. Natural size.

Fig. 7. Alitrocaprina tschoppi. Posterior view of bivalve specimen {Ca 92), which grows upon the
posterior side of an Antillocaprina annulata (Ca 62, left valve), seen from the umbo towards the commissure,
with the concave dorsal side down. Note thick outer shell layer of right valve of the Mitrocaprina. ± X 4, 5.

Fig. 8. A. pugniformis. Right valve (Ca63). Showing the S, a deep depression and the still deeper E.
The two sections (lower and top) have been given on PI. 1, ff. 6, 7. ± X 4/5.

Fig. 9. A. annulata. Section through the right valve (Ca 54). For the cardinal details see PI. 1, f. 3,
a reduccd copy of which is given on PI. 3, f. 2. A detail of this scction is figured on PI. 9, f. 2. Note
the difference between thick-walled and thin-walled canals. Natural size.

Fig. 11. Antillocaprina aff. gen. B. (W 132). With flange-like ribs. The top section has been figured
on PI. 2, f 8. i X 2/3.

Fig. 1. Titanosarcolites giganteus (Whitfield). Horizontal section through Ca 70. With strctchcd canals
in the muscle area's and three deep grooves at the siphonal region. A rcduced drawing of this section
has been given on Pl. 2, f. 5. Natural size.

Fig. 2. Antillocaprina annulata (Palmer). (Ca54). Detail of Pl. 8, f. 9. An' with undulated outline;
ma with smaller canals. Dorsal area of small canals faintly visible directly above An'. Several of the canal-
walls have split up along the median plane. X 5.

Fig. 3. Antillocaprina crassitela n. sp. (W 115.1). Detail of Pl. 8, f. 6. Note thick canal-walls ; fibrous
ligament; extremely thin bottle-neck of Piy', and a transverse tabula in Piv'- X 6.

Fig. 4. Antillocaprina annulata juvenilis (Ca 58). For explanation see Pl. 1, f 1 where a drawing of
this photograph has been given. X 34.

Fig. 1. Torreites tschoppi n. sp. (Ca 160, cotype). Upper view of feature-less left valve, L and S
well, E faintly visible. Natural size.

Fig. 2. Vaccinites inaequicostatus macgillavrji (Palmer). (CallO). With coarse ribs, slightly elevated
left valve and undulated commissure, faintly visible above the section. The section has been given on
PI. 4, f. 6. X 1/2.

Fig. 3. Praeharrettia corrali (Palmer). (Ca 187). The precense of pillars is indicated by grooves on
the exterior. The surface between grooves is covered with riblets. X 1/2.

Fig. 4. Torreites tschoppi n. sp. (Ca 160, type colony). A colony of two specimens, with a young
uncomplete specimen clinging to them (faintly visible in the middle of the figure near the bottom). X 1/2.

Fig. 5. Parastroma guitarti (Palmer). (Ca 120). Photograph of the reticulate pores, which, when
eroded, become rectangularly denticulate. This marvellous specimen was collected by Dr. Tschopp. X 2.

Fig. 7. Horizontal scction with the periphery to the left. The conccntrical nature of the structure
is evident.

Fig. 8. Tangential scction. The true tangential direction, normal to the shell's radius, is rcachcd
to the extreme right of the figure. Towards the left the section is nearing the periphery.

Fig. 9. Radial scction. Note narrowing of the folds towards the periphery (left).

Fig. 10. Horizontal scction. The structure is scarcely concentrically (vertical direction) arranged.
In accordance with that, there is no difference between the tangential (fig. 11) and radial (fig. 12) section.

j^i-'-'ixi''.■•■.■■'.•nbsp;' ■ quot;nbsp;■'■fei •nbsp;' •'■•-..

Wanneer het bestaan van convectie stromingen in het
substratum van de aardkorst aangenomen wordt, is een
isostadsche reducde volgens een der systemen, uitgaande
van een topographie ten opzichte van zeeniveau, niet
meer juist.

De gabbro intrusies op Cuba moeten beschouwd worden
als difFerentiaten van het peridotiet magma.

De binnen- en buitenlaag van Rudisten komen niet
overeen met de zogenaamde binnen- en buitenlaag van
de anorganische schaal van sommige andere Lamelli-
brancliiata.

Ten onrechte wordt in vele leerboeken bij de bespreking
van de schaalstructuur der Lamcllibranchiata Anodonta als
voorbeeld genomen.

De verdeling van het aantal terrassen per eenheid van
hoogteverschil wijst veeleer op een verdeling volgens de
waarschijnlijkheid, dan op een oscillatie van het land ten
opzichte van het zeeniveau.

Het bestaan van een breuk, lopende door het dal van
Arangjelovac, Sumadija, Jugoslavie, kan zowel op geomor-
phologische, als op geologische gronden aangetoond worden.

Een grotere of geringere rijkdom aan kali-veldspaat
mag niet als uiteindelijk criterium gebruikt worden voor
de onderscheiding van de zogenaamde oude en jonge
granodiorieten van Zuid Amerika.

De hypothese van appositie en resorptie bij de ver-
plaatsing van de spieren gedurende de schaal-groei wordt
voor Nautilus op onvoldoende gronden verworpen.

De hypothese van appositie en resorptie bij de ver-
plaatsing van de spieren gedurende de schaal-groei wordt
voor de Lamellibranchiata op onvoldoende gronden aan-
genomen.

De tegenwoordige inrichting der entomologische collec-
ties maakt faunistische studies ondoenlijk.

Het voorkomen van de Cicindeliden (Insecta, Coleop-
tera) op de kleine bovenwindse Andllen, toont aan, dat
deze dieren zich in zeer recente tijd verspreid hebben,
toen de configuratie van het land ongeveer gelijk was
aan de tegenwoordige.

tuff series; l:intercalated limestone (middle cretageous)
aptychi limestones clowermost gretageous)
geological boundary.
faults.

Distance L—CV	Douvillé fig. cit.:	7
Distance An—Piv'	Whitfield PL 21 :	25
Distance An'—CV	Whitfield PL 21 :	11
Distance between CV and
undefined alveole:	S 69:	7
Distance Piv' CV	Catadupa :	0,5

(W 64)	other samples
0,6 max.	2,2 max.	Catadupa
0,25	0,4	Catadupa
0,05	0,12(0,07	-0,2)Catad.
	1,5 min.	Catadupa
0,7 (dorsally amp; ventrally)
	0,7	Ca 68
	0,7	Ca 69
	1,2	Ca 70
0,04—0,1	0,15	Ca 70
0,5	0,7	S 65
1,7	2,6	S 65

macgillavryi Ca 96	1/3,5	70	35	190	16 15
Ca 97	1/3,2	100	40-45	170	15 17
Ca 98	1/4	■ 70		—	13 10
Ca 99	1/3,6	90	35	215	15 15
CalOO	1/3,7	95	—	—	11 15
CalOl	1/3,6	75	(50)	(180)	25 24
Cal02	1/5	50	40	200	11 14
Cal03	1/3,9	(75)	50	185	13 17
Cal04	1/4,4	60	25	180	15 18
Cal05	1/4,2	65	—	_	13 16
Cal06	—	—	_	_
Cal07	1/4,5	65	—	_	15 20
Cal08	1/3,1	95	45	185	20 19
Cal09	1/5	50	40	165	13 12
CallO	1/3,5	75	35	185	18 18
Calll	1/4,3	55	30	—	16 15
Call 2	1/4,2	80	(45)	(180)	20 19
Call3	(1/3,6)	70	(40)		15 15
Call4	1/3,2	(95)	(40)	—	21 22
Call5	1/2,9	90	(40)	(210)	24 17
Call6	(1/4)	65			18 16
Call 7	1/4,8	65	35	180	16 10
cf macgillavryi W 12	1/5	40	30	180	21 14
vermunti W 10	_	85	(45)		33 28
W 11	(1/3,4)	85	40	190	22 19
—	1/2,9	105	50	200	30 22
inaequicostatus
Gösau Douv., PI, 30, 3	1/4,2	65	20	190	13 14
Toucas, f 172	1/5	(40)	20	(210)	—
Oberberg Dv,, PI, 30,4	1/6,4	15	35	170	gt;
SironeDv., PI, 30, 5	1/3,4	75	_	_
Dv,, PI. 33, 2	1/4	70	—	_	gt;
Dv., PI, 33, 3	1/5	50	15	195
Aless., PI, 14, 5	(1/5)	45	(20)
Aless., PI. 16, 5	1/4,2	85	25	(180)
Leposavici Mil., f. 2	1/3,7	80	—		=

	r: u	L\JE	APyL	APyPm,
macgillavryi Ca 96	1/3,5	70	35	190
Ca 97	1/3,2	100	40—45	170
Ca 98	1/4	70	—	_
Ca 99	1/3,6	90	35	215
CalOO	1/3,7	95	—
CalOl	1/3,6	75	(50)	(180)
Cal02	1/5	50	40	200
Cal03	1/3,9	(75)	50	185
Cal04	1/4,4	60	25	180
Cal05	1/4,2	65	_	_
Cal06		_	_	_
Cal07	1/4,5	65	_	_
Cal08	1/3,1	95	45	185
Cal09	1/5	50	40	165
CallO	1/3,5	75	35	185
Calll	1/4,3	55	30	—
Call2	1/4,2	80	(45)	(180)
Call3	(1/3,6)	70	(40)
Call4	1/3,2	(95)		_
Call5	1/2,9	90	(40)	(210)
Call 6	(1/4)	65
Call 7	1/4,8	65	35	180
cf macgillavryi W 12	1/5	40	30	180
vermunti W 10	_	85	(45)
W 11	(1/3,4)	85	40	190
—	1/2,9	105	50	200
inaequicostatus
Gösau Douv., PI. 30, 3	1/4,2	65	20	190
Toucas, f. 172	1/5	(40)	20	(210)
Oberberg Dv., PI. 30,4	1/6,4	15	35	170
Sirone Dv., PI. 30, 5	1/3,4	75	_	_
Dv., PI. 33, 2	1/4	70	—	_
Dv., PL 33, 3	1/5	50	15	195
Aless., PL 14, 5	(1/5)	45	(20)
Aless., PL 16, 5	1/4,2	85	25	(180)
Leposaviei Mil., f. 2	1/3,7	80	-

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