■ f

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 22 MAART
1937, DES NAMIDDAGS TE 4 UUR

DEZE DISSEIITATIE VERSCHIJNT TEVENS ALS No. 13 VAN DE I'HYSIOGRAI'HISCH-
GEOLOGlSCHE REEKS DER GKOGRAPHISCHK KN GI-OLOGISCHI: MKDKDKELINGKN

Het is mij een behoefte U, Mooglceraren in de Facukeit
der Wis- en Natuurkunde, van wie ik mijn weten-
schappehjke opleiding mocht ontvangen, aan het einde
van mijne academische studiën, mijn dank tc betuigen.
Dit geldt in de eerste plaats mijn Promotor, Prof. Dr.
L. Rutten.

General; Western part; Age of the Limestone
Hills; Position of the hmestones in the Western
part; Chert zone; Eastern part; Age of the
Eastern part; Pétrographie description of the
rocks of the San Andres formation.

General; Age; Pétrographie description of
Serpentine rocks; Inclusions of unknown
origin; Gabbroid dikes.

General ; Age ; Eastern facies ; Description of
rocks of Eastern facies ; Mountain facies.

■

! v.-'!

An expedition of the Utrecht University made a geological survey of
different parts of the isle of Cuba during the spdng and the summer
of 1933. The members of this expedition were, the leader Prof. L. M. R.
Rutten, Mrs. C. J. Rutten-Pekelharing, Miss A. Röntgen and the
following students of geology at the Utrecht University, Dr. M. G.
Rutten, Mr. H. J. Mac Gillavry, Dr. A. A. Thiadens, and the author.

From the 18 th of May undl the 9 th of July, we worked in the Western
part of Cuba, the province of Pinar del Rio. From the central camps, pitched
in the tov/ns of Pinar del Rio, San Diego de los Banos, San Cnstobal, the
members worked in different directions, whereas small pardes consisting
of two members surveyed the neighbourhood of Alatahambre La
Esperanza, Bahia Honda, Cacarajicara (South West of Bahia Honda),
Cabanas, Matiel. The busy traffic along the Carretera Central, Cuba's
highway running along the axis of the island, enabled us to work even at
large distances from the central camps. All notes made and all matenal
collected by the members of the expedition in Pinar del Rio province were
turned over to the author, who worked out the data in this paper.

For general onentation in the field we used military maps, kindly put
at our disposal by the Cuban government. These maps, (scale 1 : 100000),
proved to be insufficiently accurate in detail, so we had to survey our own
roads. This was done by taking direction with a hand-compass and
measuring the distances by counting our paces. The map constructed in
this way proved to be more reliable than the military maps and sufficiently
correct to sketch in our rough geological survey. A detailed geological
survey would be impossible without reliable topographical maps.

In the laboratory at Utrecht wc used as a basis for the construction of
our map the nautical charts of the United States Navy. As fixed points were
taken the towns of La Coloma on the Southern coast and Santa Lucia,
Puerto Esperanza, Verracos, Puerto Blanco, Bahia Honda, Cabaiïas and
Matiel on the Northern coast. As the reader will see, La Coloma is not to
be found on our map. Wc knew, however, by pacc-compass survey, the
relative position of the town of Pinar del Rio with regard to La Coloma.

Wc further had at our disposal a special map of the Carretera Central.
The direction of the road on this special map greatly differed from the
direction of this same road on the military map, e.g. the town of Santa
Cruz dc los Pifios is situated about 12 km to the North on the latter. We
could chcck the directions of the Carretera Central at various places and
as our observations tallied more or less with the military map, we ignored
the special map of the highway.

Between the fixed points copied from the U.S. navy chart we mapped
down our own surveys. The correction necessary between La Coloma
and Puerto Esperanza, was an enlargement of our survey by 6 %. Other
corrections were made with the help of the triangles formed by the roads.
Several roads were surveyed on horseback. Direction was taken by hand-
compass as usual, but the distances were judged at an estimate. This judging
of distances proved to require a large experience, especially on the winding
mountain roads, and grave errors were made. The survey on horseback,
however, was necessary in those parts of the Organos mountains, which
were practically uninhabited and large distances had to be covered in one
day. On account of the unreliability of the distances of our horseback
surveys, we attached only a secondary importance to them when drawing
our map.

We prepared two maps, a geological coloured one and another on
which the findspots of fossils and rocks are marked. The geological boun-
daries are also indicated on the latter, in order to facilitate the comparison
with the former.

On all the roads sketched in on the map geological observations were
made, with the exception of the Carretera Central, which was only partly
surveyed. The closeness of the network of our observations and the places
where the geological interpretation is unsupported by observations are
therefore clearly visible on the map.

Several regions in Pinar del Rio province could not be visited by us
on account of lack of time. One of these regions, the reconnaissance of
which is essential in order to understand the geology of Pinar del Rio
IS between the towns of San Diego de los Bafios and La Mulata. Between
Quiebra-Hacha and Cayajabos we left a space blank on the map as two table
mountains were seen in this area from some distance. The notable difference
of morphologic aspect between the low hills of the Upper-Cretaceous-
Lower-Tertmry regions and the table mountains, indicates the possibility
that other formations are exposed there. The region of the blank space
on the map West of Cayajabos, seems to be built up predominantly of
limestone hills of the same kind as those which are found to the West
The region between Viiiales, iMatahambre and Sumidero may be expected
to consist of hmestone quot;Mogotesquot; and phyllite/quartzite rocks

The region between Matahambre, Santa Lucia and La Esperanza
has been marked upon the map as San Andres formation. Two members
of our expedition passed through this region, noting in general the

To Prof. Dr. L. M. R. Rutten, the leader of our expedition, whose
large experience in field-work and whose support when treating the various
geological problems in this paper, have been of inestimable help to me.

To Mrs. Dr. C. J. Rutten-Pekelharing, whose powers of endurance
and cheerfulness on the frequently long and arduous trips, served us all
as an example.

To my colleagues H. J. Mac Gillavry, M. G. Rutten, and A. A.
Thiadens. The excellent mutual understanding contributed largely to the
success of our trip.

The quot;Molengraaff-Fondsquot; and the quot;Bataafsche Petroleum Maatschappijquot;
for their pecuniary aid to our expedition.

The Cuban Government and the Sociedad Geografica de Cuba which
rendered us every possible assistance.

Mr. poliakoff of the Compania Shell Mex., whose valuable help
very much has been appreciated.

Dr. Tschopp, geologist of the Shell Mex., whose kindness in discussing
the geological problems of Cuba cannot be too highly esteemed.

Prof. Dr. J. I. J. M. Schmutzer for his assistance on revising the
microscopic thin-sections.

Prof. Dr. F. Trauth of Vienna and Prof. Dr. E. Jaworski of Bonn,
who were so kind as to undertake respectively the study of the Aptychi
and Ammonites, collected by us in Cuba.

Mr. J. van Dijk, of the Utrecht Laboratory, who executed with great
accuracy the drawings and micro-photographs reproduced in this paper.

Further I should like to say, that during our stay in Cuba, wc met with
nothing but the greatest hospitality and kindness from the side of the Cuban
people, and I wish to express my gratitude to them.

The oldest rocks exposed in the province of Pinar del Rio are sandstones,
quartzitic sandstones, quartzites, slates, phyllites, cherts and limestones.
We name this series of rocks the San Andres formation, thus combining
the Cayetano formation and the Vinales limestones, both names introduced
by de Golyer (28). The limestones are partly of Upper Jurassic, partly
of Lower Cretaceous age; moreover, we take them to be intercalated in
the quartzite-phyllite formation. We cannot differentiate the greater part
of the limestones in Upper Jurassic and Lower Cretaceous strata as paleon-
tological evidence is often wanting. Also for this reason we suggest a new
name, including the Cayetano formation, until a minute survey will produce
evidence justifying a more detailed division. The formation has been named
after the village of San Andres, situated in the centre of the wide-spread
mountain area, where this formation is exposed.

The San Andres formation can be divided into two parts, respectively
found East and West of the town of San Diego de los Banos. In the Western
part quartzitic and phyllitic rocks (rocks of Cayetano facies) are predominant.
Cherts and limestones of Upper Jurassic and Lower Cretaceous age are
intercalated. The Eastern part consists chiefly of limestones with minor
intercalation of rocks of Cayetano facies. The age of part of the limestones
is Lower Cretaceous on account of Aptychi found at various places. These
beds are the equivalent of the ./l/^-rZ»/limestones of the Santa Clara province
described by M. G. Rutten (64). Brown and O'Connell (12) mention the
occurrence of Jurrassic Ammonites in the Eastern region, consequently
older beds, e.g. Upper Jurrassic, may be developed.

Following the sedimentation of the strata of the San Andres formation
begins volcanic activity, resulting in the deposition of the Tuff Scries.
These strata consist of porphyrites, diabases, vitric-tuffs, tuflites, tuff-brcccias,
Radiolaria bearing cherts and grayish-blue well bedded limestones. The
latter are especially developed in the lower parts of the Tuff Series. The
age of the Tuff Scries is uncertain, as no fossils were found in the beds
exposed in the province of Pinar del Rio. They are post-Lower Cretaceous,
as they rest conformably upon the younger parts of the San Andres for-
mation and pre-Upper Cretaccous (Macstrichtian of Europe) as they are
unconformably covcrcd by the beds of the Habana formation.

The orogenctic phase, which followed the sedimentation of the Tuff
Series, folded the San Andres formation and the Tuff Scries to a large
anticline. During this orogenesis, harzburgites, gabbroid dikes and dioritic
rocks intruded. The harzburgites, at present for the greater part serpentinized.

carry inclusions of rocks partly derived from the Tuff Series (porphyrites
and diabases) and rocks of unknown origin (amphibohtes, actinolite-schists
and hornblende-plagioclase rocks).

After a period of denudation, the Habana formation was deposed
disconformably upon the older formations. These strata of Upper Creta-
ceous age (Maestrichtian of Europe) are characterized by the occurrence of
Rudists and Orbitoids. The Habana formation is developed in two different
facies ; the quot;Mountain faciesquot; and the quot;Eastern faciesquot;. The former is
exposed in the mountain regions, the latter to the North, East and South of
them. The rocks of the Mountain facies are dark-blue limestone breccias
and conglomeratic sandstones. The rocks of the Eastern facies consist of
conglomerates, white to brown calcareous sandstones, marls, chalks and
white limestones. These beds cannot be distinguished from the Upper
Eocene and Ohgocene strata, when paleontological evidence is lacking.

A regression and possibly an orogenesis followed the sedimentation
of the Habana formation, as the Lower Eocene is not developed in Pinar
del Rio. The Upper Eocene is only found in the belt of younger sediments
around the mountain regions ; so we assume that after the deposition of
the Upper Cretaceous, the central regions rose, thus preventing the pene-
tration of the Upper Eocene transgression.

The Upper Eocene and Oligocene layers consist of white limestones,
conglomerates, calcareous sandstones, white marls and chalks.

A renewed orogenetic activity took place after the deposition of the
Ohgocene beds. These orogenetic phases wedged the Habana formation
of Mountain facies into the older formations, whereas the Habana formation
of Eastern facies and the Upper Eocene and also the Oligocenc beds were
strongly folded.

Then follows the sedimentation of the Oligomiocene beds consisting
of white or brown limestones (equivalent of the Guinness limestones)
carrying an abundant and constant fauna oî Foraminijera, red sands and
purple days The Ohgomiocene beds are found in horizontal position or
with slight dips. The last post-Oligomiocenc orogenetic phase must have
been of small importance and even locally absent as large areas arc covered
with horizontal Oligomiocene beds.

The San Andres formation forms the greater part of the mountain
regions in the province of Pinar del Rio. It consists of phylhtes, slates,
quartzites, sandstones and marbles, which were called the Cayetano
formation by de Golyer (28), and of massive grayish-blue limestones
formerly called the Vinales limestones often cut by thin calcite veinlets.

Moreover, grayish-blue, thin-bedded limestones are found. In the
quartzitic and phylhtic beds, which we shall call rocks of quot;Cayetano faciesquot;
and in the limestones, we find intercalations of cherts.

The limestones are a typical feature in the landscape, especially in the
Western part of the Organos mountains. They form steep, often isolated
hills, called quot;Mogotesquot; in Cuba, between which we find a red soil or rocks
of Cayetano facies.

We can divide the region, in which the San Andres formation is
found, into two distinctly different parts; the boundary between these parts
running from near the town of San Diego de los Bafios to the North. West
of this boundary we find the rocks of Cayetano facies dominating, the
outcrops of limestones are in the minority. The Eastern part consists
chiefly of limestones, often well bedded, with occasional intercalations of
quartzitic rocks of Cayetano facies.

This contrast between the Eastern and Western region is difficult to
explain. Brown and O'Connell (12) advancc the opinion, that the older
strata are stronger developed in the Western part, which in our opinion
may be the case, as Upper Jurassic fossils, often found in the Western part,
were not met with by us in the Eastern part. Apart from the possibility that
strata of different ages are found in the two regions, change of facies is also
in all probability of great importance. It may accentuate the difference
between the two regions. In the transsitional area we have to our great
regret insufficient observations to offer a definite solution of the interesting
problem.

We introduce the new name San Andres formation, thus combining
the Cayetano formation and the Viiiales formation.

De Golyer (28) considers the Cayetano formation to overlie the
Vinales limestones. Me mentions limestone-intercalations at the base of
the Cayetano formation. The limestone hills near Sumidero quot;may be part
of the Vinales limestones brought up by faulting rather than a part of the
Cayetano formation.quot;

Brown and O'Connell (12) take the Cayetano formation to lie
unconformably under the Vinales hmestones, to which they ascribe an
Upper Jurassic age.

Dickerson and Butt (30) in a recent pubhcation accept the unconfor-
mity between the Cayetano formation and the Vinales limestones, but take
the Ammonites on which the Upper Jurassic age of the Vinales hmestones
is based by Brown and O'Connell (12), to be derived from the Cayetano
formation, which consequently is of Upper Jurassic age in their opinion.
The Vinales limestones and the Eastern part of the Organos mountains
are reckoned to be of Lower Cretaceous age on account of Ammonites and
Aptjchi found at La Catahna and on the trail between San Cristobal and
El Rosario.

In our opinion the limestones are partly of Upper Jurassic, partly of
Lower Cretaceous age; moreover we take them to be intercalated in the
quartzite-phylhte formation (Cayetano formation). As we cannot differen-
tiate the greater part of the limestones in Upper Jurassic or Lower Cretaceous
strata, we suggest a new name for a formation which then includes the
Cayetano formation, until a minute survey will produce evidence, justifying
a more detailed division.

A large area of quartzitic and phyhitic rocks runs South of the limestone
hills from the town of Guanc in the West to San Diego de los Banos in
the East. Though these strata are strongly folded, the structure of a large
antichne is clear. The Northern and Southern flanks of this anticline are
especially evident South East of Luis Lazo, North West of San Juan y
Martinez, on the road from the town of Pinar del Rio to Sumidero and
South of San Andres. In this zone of rocks of Cayetano facies we find
intercalations of marbles and of grayish-blue limestones. North West of
the town of Pinar del Rio and North of Consolacion del Sur. At the Northern
boundary of this large district of rocks of Cayetano facies. we find the
limestone quot;mogotesquot; separated from each other in some cases by broad
strips of rocks of Cayetano facies and limited in the North also by rocks
of Cayetano facies.nbsp;^

Age of the Limestone Hills: The quot;mogotesquot; consist of a
compact grayish-blue limestone, often cut by small calcite veinlets and
dark shales. They rise steeply out of level plains, which are for the trrcitcr
part covered by a red soil This quot;mogotequot; landscape is typically deve-
loped in the neighbourhood of Vinales.nbsp;^^ ^

In some places, at the foot of these hills we find the Ammonite bearing
limestone concretions, which are called quot;quesosquot; by the peasants on acrnn J
of their form. The best known findspot of these 'gt;eso? squot; uated S
of the town of Viilales at the Puerto Ancon, was dis^covered quot;carl^

de la Torre (76), who ascribed a Jurassic age to the Ammonites found in
them. Later pubhcations of Sanchez Roig (67) and Brown and O'Connell
(12) corroborated this determination; the limestones and shales, from
which the Ammonite bearing concretions were considered to be derived,
were placed by them in the Oxford.

Brown and O'Connell (12) mention two new findspots of Ammonites,
namely, San Vicente and Mina Constancia. In both localities the strata
from which the fossils are derived, are considered to be of Jurassic age.

We collected Ammonites, South East of Guane at loc. V. 585 and at or
near the Puerta Ancon. The preliminary examination of this material by
Jaworski (not yet published) also points to an Upper Oxford or Lower

Dickerson and Butt (30) mention further localities where Jurassic
Ammonites are found, e.g. at the East foot of the Sierra San Carlos, about
two km North of the setdement of Punta la Sierra (between Guane and
Sumidero) at the South foot of the Sierra La Abra (South of San Cayetano),
and in the neighbourhood of La Jagua Vieja (South East of La Esperanza).
As already mentioned, they take the concretions to originate from the
quartzitic and phyllitic rocks. We think it highly improbable that the
Ammonites should occur in the rocks of Cayetano facies only in those
places, where, in Dickerson and Butt's opinion the limestones cover
even unconformably, those rocks. A second and conclusive argument
against Dickerson and Butt's opinion is the fact that, e.g. at the classical
findspot Puerto Ancon, the concretions with Ammonites are found on the
debris slope of the limestone hills and moreover North of a zone of rocks
of Habana formation, found somewhat to the West, which marks the
anomalous contact between the limestones and the rocks of Cayetano
facies. Lastly, the beds of Cayetano facies do not outcrop, at the findspot

At loc. L. 894 situated North West of San Diego de los Bafios and
near La Catalina, we collected Ammonites in distincly northward dipping
limestones, intercalated in rocks of Cayetano facies to which Jaworski
ascribes an Upper Tithonian or more probably Valanginian age. Dickerson
and Butt mention the occurrence of Lower Cretaceous Ammonites and

■ Resuming we find that the limestones found in the Western part of the
San Andres formation are partly of O.xfordian-Kimmeridgian partly of

Owing to the complicated tectonical structure and die scarceness of
fossils in the limestones, we did not try to separate the hmestones of dif-
ferent ages on the map. Moreover they are sketched-in roughly.

Position of the limestone beds (Western Part)y\s already
mentioned Brown and O'Connell (12) and Dickerson and Butt 30)
consider the limestones to cover unconformably the quartzitic and phylhtic

rocks We do not agree with this opinion. We have evidence of intercalated
.mestones in the rocks of Cayetano facies West of San Diego de los Bafios
at Iocs. V 675 and V. 680. These limestones are compact, blueish gray of

outcrops of a transgressive formation of Upper Cretaceous age; they are
often associated with small strips of serpentines and occur near the large
limestone hills. These Habana beds of quot;Mountain faciesquot; are described
on p. 25. These transgressive beds lie in anomalous contact with the older
formations. The serpentine seems to have acted as a quot;shde-expedientquot; on
which overthrusting took place. Strike and dip are not to be measured in
the breccious or conglomeratic Upper Cretaceous beds, but their position
at the foot of the large limestone hills in the generally North dipping
beds of the San Andres formation points to overthrusts. The anomalous
contacts were not indicated as such upon the map, because the small
occurrences of the Upper Cretaceous layers, already exaggerated on the
map, would become wholly invisible.

Resuming we take the phyllitic quartzitic rocks and the limestones
to belong to a continued sedimentation cycle in Jurrassic to Lower
Cretaceous time. After a period of orogenetic activity, followed by denu-
dation, the Upper Cretaceous transgression covered these regions. During
a post-Maestrichtian orogenesis overthrusting took place.

Chert Zone: Intercalations of chert are found in the quartzitic
phyllitic zone and in the limestone strata. A large area of cherts, however,
was found between San Cayetano and La Esperanza. The trail which runs
East from La Esperanza and then to the South, also crosses this chert zone
between the Iocs. L. 1018 and L. 1020. It is also found South of Verracos.
The thin bedded cherts, varying from yellow-gray to black in colour often
carry Radiolaria. The strata arc strongly folded in detail. They are reckoned
by us to belong to the San Andres formation.

In contradistinction to the Western part limestones dominate in the
mountain regions East of San Diego de los Banos. Rocks of Cayetano
facies are so in the minonty, and the outcrops of such small dimensions,
that we did not put them down on the map. When found, however, the
quartzites or quartzitic sandstones are in general appearance and in thin
sections practically identical with the rocks found in the Western parts.
The strata further consist of black or violet shales, cherts often carrying
Radiolaria, and caicarcous sandstones. The limestones arc from light to
dark blueish-gray in colour, and mostly thin-bedded. They are more of less
crystalline.

The strike of the beds runs in general in East Western direction,
dipping to the North; at the Southern part of the area where the San Andres

The strata of the San Andres formation are covcrcd in the North by
the beds of the Tuff Series. The Southern boundary is a large fault which
is based chiefly on morphologic arguments (the abrupt ending of the

mountain region). Outcrops of the belt of younger sediments are scarce
Between the Ohgomiocene beds and the rocks of the San Andres formation
the area which is left white on the map, is either without any outcrops or
covered by alluvial deposits of which the large boulders are partly derived
from the San Andres formation.

North of Guanajay occurs another area of rocks, which are similar
to the rocks of the Organos mountains. Contrary to the latter it is a flat
country, with only low hills. The strata consists of blueish-gray and greenish-
gray, weH bedded hmestones, often cut by small calcite veinlets, of cherts
and of violet shales.

Age of the San Andres formation Eastern part: In several
ocahties (V. 868, A. 653, V. 826) Aptychi were collected by us in the
limestone beds. They were studied by Prof. Trauth (79), who ascribed a
Lower Cretaceous age to them. At loc. V. 868, South of Bahia Honda
Ammonites were coUected with the Aptychi. They are, however in all
probabdity in too bad a state of preservation for determination. Brown
and OConnell (12) mention the occurrence of Ammonites, which thev
consider to be of Upper Jurrassic age at localities North of Candelaria and
. unbsp;this last locahty they collected, however, also

Aptychi, the resemblance of which with Lower Cretaceous species has been
already pointed out by them. Dickerson and Butt (30) also collected Aptychi
and Ammonites on the trail between San Cristobal and EI Rosario, w4h
are considered to be of Lower Cretaceous age.

Ru^en (64) described from Northern sLta Clara, and will be deS
by Mac Gillavry (in litt.) from Camagueynbsp;described

With regard to the age of rocks of Cayetano facies we mention the
occurrence of a quartzitic sandstone, noted but not sampled, Tnte caquot;aS

As in the Western part, numerous overthrusts, indicated bv (he '
occurrence of Maestnchtian beds (Habana formation of Mou^ fLiS

or angular of shape and either polluted or clear. Occasionally twinned
plagioclase of acid composition (albite) occurs. The mica is a colourless
muscovite developed as small or larger plates. The plates are either irre-
gularly arranged or show a linear structure. The matrix is a greenish-brown
limonitic substance. In rocks grading into quartzitic sandstones the amount
of matrix is small.

Quartzitic sandstones: The rocks consist of the same constituents
as the sandstones. The quartz is clear, rounded or angular and in places
shows a sutured texture. The limonitic matrix is often replaced by thin
sericite layers, accentuating the foliated structure. The twinned albite
crystals and the muscovite plates are occasionally bent, due to tectonical
stresses. In some rocks the plagioclases are sericitized. As accessory niinerals
we find zircon and tourmaline. The quartzitic sandstones form with the
quartzites a prominent part of the San Andres formation.

Quartzites: Quartzidc rocks are medium to coarse-grained and white-
gray to grayish-brown or red-brown in colour. Under the microscope the
rocks consist of clear quartz crystals, strongly intergrown with each other
and of sericite. The sericite occurs in thin layers or patches. It is often
mixed with a limonitic substance and with fine ore grains. Muscovite is
developed as small or large plates. The plagioclase crystals, which are
nearly always found in small quantities, arc of acid composition (albite).
Accessory minerals are zircon and tourmaline.

The texture of the rocks varies. Part of the quarzites show a linear
arrangement of the muscovite plates or the sencite layers; the quartzes of
these rocks, though often showing strain-shadows, are irregularly arranged.
Other rocks, however, show apart from the linear arrangement of the
micaceous elements, a distinct parallelism of the quartz crystals. Part of
the rocks, we called quartzites, thus grade into the higher metamorphic
sericite-quartz schists. Taking into consideration, that non-metamorphic
sandstones occur besides quartzites and sericite-quartz schists, it is probable
that tectonical stresses had an influence upon the rocks apart from the
regional metamorphism.

Slates: Slaty rocks often occur in the San Andres formation. They arc
fine grained and of light grayish or purple colours. Foliated structure is
pronounced. Fresh rocks are diflicult to obtain, because of the easy weathe-
ring. In thin-sections the rocks consist of fine quartz dust in a matrix ot
chlontic limonitic substance. Small twinned plagioclasc laths are found.
Sencite occurs in changing quantities. In cases, the matrix is a dark red-
brown mass, consisting probably of hematite. Small cubi of pyritic ore
are often found.

Phyllites: True phyllitic rocks arc found considerably less than the
slates. The lustrous rocks arc rcddish-purple or grcenish-gray. Under the

microscope the rocks consist of strongly intergrown quartz patches, shaped
as lenticles or small bands, conforming with the parallel arrangement. The
sericite layers between the quartz patches are often mixed with a limonitic
substance.

Limestones: Several authors e.g. Lewis (44) and Dickerson (in
private correspondence with Prof. Rutten), pointed to the difference of
the highly crystalline marbles intercalated in the quartzite-phylhte beds
and the less crystalline quot;Mogotequot; limestones. We already discussed the
fact that quartzitic rocks occur in the limestone hills. As regards their
metamorphism these rocks do not differ from the rocks found in the large
quartzite-phylhte areas. With regard to the limestones, which are macros-
copically often difficult to separate, we made several thin-secdons in order
to examine the state of crystallization of the different rocks. We can dis-
criminate fine-grained crystalline rocks and coarse crystalhne limestones.
The latter show different stages of crystallizadon. Some rocks consist of
idiomorphic calcite rhomboeders, which in other rocks pass into allotrio-
morphic calcite crystals. Transitional phases are found. In cases the old
contours of the rhomboeders are visible in the coarse calcite crystals (loc
V.710, North of San Diego de los Banos). The limestones occasionally
show a hnear structure, accentuated in the fine grained rocks by the
polluted parts and in the coarse crystalline limestones by the parallel
arrangement of the calcite crystals.

With regard to the occurrence of the fine-grained and coarse crystalline
limestones, we find the coarse crystalline rocks also in the quot;xMocotesquot;
and in the Eastern part of the Organos mountains, and the fine-grained
hmestone intercalated in the quartzite phyllite strata. Outcrops of crystalline

L. 770 Both locahties seem to belong to the same level. The extreme
crystalhne marb es found at loc. L. 780, North of the town of PinarTel
Rio, are generally taken as the prototype of the intercalated limestones in
he quartzite phylhte formation. They are indeed the strongest cry^^al ine
limestones, we found in the Province of Pinar del Rio. The lime ^es
found at loc. A. 619 West of loc. L. 780, in all probability can be ~
with the marWes ; tl^y are considerably less cUnine.'ln the nekS

»00, L. »58 and V. 703. Coarse crvsta ine 1 meston^c or« f j
L. 853 and V. 7,0. We have no reasonl diffe entTateXquot;u^ quot; •
above on account of a different position.nbsp;mentioned

The examination of the material we have at our disposal nmv.. .1 ,
there .s no contrast between fine-grained quot;Mogotequot; limSa';;d Itronjequot;

metamorphic hmestones intercalated in the quartzite phyllite beds. Both
kinds occur in either of them.

Suboohtic hmestones are found at loc. H. 812, North of Consolacion
del Sur and loc. V. 547, North East of Consolacion del Sur. The fragments
of suboohtic limestones found in the breccia-limestones of the Habana-
formation of Mountain facies resemble these limestones.

Fine-grained dense limestones, carrying Radiolaria are found at loc.
H. 834, North East of San Andres and at loc. L. 916, North of Candelaria.

The characteristic elements of this series are porphyrites, diabases,
glass tuffs, tuff breccias and tuffites, alternating with blueish gray well
bedded limestones, cherts and shales. We find these beds exposed at the
Northern side of the younger part of the San Andres formation East of
San Diego de los Bahos. The Tuff Series beds cover these younger parts of
the San Andres formation (equivalent of the Lower Cretaceous Aptychi
limestones described by M. G. Rutten (64) from Northern Santa Clara)
conformably, which is clearly shown on the trail South of Bahia Honda,
where the boundary between the Tuff Series and San Andres formation
runs about 3 km North of an Aptychi findspot (loc. V. 686) in the latter.
The strikes of the beds of the Tuff Series and of the beds of the San Andres
formation run W—E the dip is constantly to the North. The association
of volcanic beds and limestones is typical for the Northern facies of the
Tuff Series in Santa Clara province. AL G. Rutten reckons the Aptychi
limestones and the lower parts of the Tuff Series to be of the same age and
only differing in facies. From our observations in Pinar del Rio wc conclude
that the Tuff Series is younger than the equivalent of the Aptychi limestones,
the younger parts of the San Andres formation. In the lower part of the
Tuff Scries, limestones are more frequently intercalated than in the higher
parts, where they even may be absent. The limestones found in the lower
part of the Tuff Series, in places contain fragments of volcanic material
(loc. L. 968, South of Cabafias). All strata containing evidence of volcanic
activity are reckoned to the Tuff Scries. In these strata we never find the
sandstones and quartzitcs typical for tlie San Andres formation.

Outcrops of Habana beds of mountain facies occur in the Tuff Scries
in the same way as in the San Andres formation, marking the overthrusts.

At the Northern side the Tuff Scries area is limited by the beds of
Habana formation of Eastern facies, described elsewhere, and by Lower
Tertiary strata.

North West of Bahia Honda the Tuff Series is found again, however,
in this region entirely without intercalations of limestones, same as on the
road from Bahia Honda to Cabafias (see map). The Tuff scries strata in this
region consist of glass tuffs, Radiolaria bearing glass tulhtcs (Iocs. V. 845,
V.849, M. 1061), porphyrites and diabase-porphyrites. In the tuffites

effusive quartz occurs at loc. M. 1066, East of Bahia Honda; the quartz
grains show corrosion rims and inclusions of groundmass. In analogy
with Santa Clara province, the occurrence of effusive quartz may point to
an Upper Cretaceous age (Habana formation) of this tuffaceous rock. On
account of the extreme scarceness of the quartz material, we hesitate to
reckon this rock to the Habana formation, however, the possibility of
the occurrence of tuffaceous Habana formation in this region must be
reckoned with. Strike or dip were not measured by us in this part of the
Tuff Series. On the map we connected both areas, but a survey of the
Eastern side of the bay of Bahia Honda will be necessary to allege this with
evidence. West of the bay of Cabaiias the possibility of the occurrence of
tuffaceous rocks was noted. Outcrops in this regions, however, are too
scarce and the rocks too strongly weathered for determination.

In the town of Cayajabos strongly folded, Radiolaria carrying cherts,
are exposed, whereas North of the town at loc. L. 930, a coarse diabase
rock is found. Both rocks are reckoned to belong to the Tuff Series, but
the cherts might easily belong to the San Andres formation.

A small outcrop of diabase rock is found at loc. M. 1013, North of
San Cristobal. We take this to be an isolated intrusion of the tuffaceous
magma through the older San Andres formation. Another isolated outcrop
of coarse diabase is found at loc. L. 870, North of La Palma.

A rock, which may be allied to those found in the Tuff Series, occurs
at loc. A. 618, West of the town of Pinar del Rio, in the quartzitic phyllitic
area. The cataclastic rock consists of crushed augites and quartzitic and
calcareous elements. A sparse amphibole crystal is found. This rock might
be connected, however, with the dioritic magma.

Age of the Tuff Series: No fossils indicating the age of the Tuff
Series have been found. On account of its stratigraphic position, the Tuff
Series is younger than the Lower Cretaceous beds of the San Andres for-
mation and older than the transgressive Habana beds of Upper Cretaceous
age (Maestrichtian in Europe).

Diabases and porphyrites: The rocks are greenish blue to grayish
green. The white felspar phenocrists found in the porphyritic rocks arc
macroscopically clearly visible as tiny white spots. In thin-sections the tme
ophitic texture of the diabase grades into the porphyritic texture of the
porphyrite. The latter have a crystalline matrix of small plagioclasc lat s
and small augite grains or a vitric groundmass. The com^^sitiorof t e
felspars forming the matrix and the phenocrists is basic (1 bradorite)
In some rocks well devdoped augite phenocrists occur besides the pS
clase. Amygdaloidal diabases are also found ; the texture irnn^i
plagioclase laths are polluted and of an acidnbsp;^aft

amygdales are filled up with calcite or with quartz and calcite. Magnetite
is found in smaller or larger quantities in the diabases and in the porphyrites.

Tuffs and tuffites: The tuffs and tuffites are principally found in
the region North and East of the town of Bahia Honda. They occur together
with diabases and porphyrites. Macroscopically, the rocks are fine-grained,
soft and easily weathered. The colour is light green or light gray. Under the
microscope we can discriminate glass tuffs consisting of glass, polluted by
a green-brown chloritic limonitic substance, with rare angular fragments
of clear plagioclase. When these fragments appear in larger quantity, the
glass tuffs grade into crystal tuffs. The tuffites often carry numerous
Radiolaria and larger crystals of clear, well lamellated basic plagioclase.
Quartz is rarely found, as already mendoned. The Radiolaria beanng tuffites
are sometimes cut by veinlets of quartz and sometimes partly silicified.
They grade into cherts.

Cherts: The cherts are green to black rocks, strongly cut by veinlets,
which in thin-sections prove to be quartz and, in exceptional cases, calcite
and quartz. The rocks are often strongly polluted by a limonidc substance,
which causes a red-brown weathering. Radiolaria occur, e.g. at loc. H. 949,
South West of Bahia Honda.

Outcrops of Serpendne or of partly serpentinized rock occur in the
regions, where San Andres formation and the Tuff Series are exposed. They
appear as small bands, following the general trend of the strata. Often, but
not always, the Serpentines are accompanied by rocks of the Habana
formadon, in which case the Serpendne seems to have acted as a quot;slide
expedientquot;, when ovcrthrusdng took place.

Only one large area of Serpentine is found between La Palma and La
Mulata. The rocks form a large flat hill, a vcry distinct feature in the land-
scape, recognizable at a large distance.

Many inclusions arc found in the Serpentines; part of these arc cleady
derived from the Tuff Series, whereas more metamorphic inclusions are of
unknown odgin. The latter arc Amphibolites, Actinolite schists and

According to M. G. Rutten (64), the contacts of the Serpentine with
the older formations in Santa Clara province arc tectonical, formed by
overthrusting. The greater part of the contacts of the Serpentine zones in
the province of Pinar del Rio, support his opinion. Several Serpentine
outcrops, found near or in the limestone hills of the San Andres formation,
are covered by or cover Upper Cretaceous limestone-breccias, the occurrence

An expedition of the Utrecht University made a geological survey of
different parts of the isle of Cuba during the spring and the summer
of 1933. The members of this expedition were, the leader Prof. L. M. R.
Rutten, Mrs. C. J. Rutten-Pekelharing, Miss A. Röntgen and the
following students of geology at the Utrecht University, Dr. M. G.
Rutten, Mr. H. J. Mac Gillavry, Dr. A. A. Thiadens, and the author.

From the 18th of May until the 9 th of July, we worked in the Western
part of Cuba, the province of Pinar del Rio. From the central camps, pitched
in the tovgt;-ns of Pinar del Rio, San Diego de los Bafios, San Cristobal, the
members worked in different directions, whereas small parties consisting
of two members surveyed the neighbourhood of Matahambre, La
Esperanza, Bahia Honda, Cacarajicara (South West of Bahia Honda),
Cabanas, Mariel. The busy traffic along the Carretera Central, Cuba's
highway running along the axis of the island, enabled us to work even at
large distances from the central camps. All notes made and all material
collected by the members of the expedition in Pinar del Rio province were
turned over to the author, who worked out the data in this paper.

For general orientation in the field we used military maps, kindly put
at our disposal by the Cuban government. These maps, (scale 1 : 100000),
proved to be insufficiently accurate in detail, so we had to survey our own
roads. This was done by taking direction with a hand-compass and
measuring the distances by counting our paces. The map constructed in
this way proved to be more reliable than the military maps and sufficiently
correct to sketch in our rough geological survey. A detailed geological
survey would be impossible without reliable topographical maps.

In the laboratory at Utrecht we used as a basis for the construction of
our map the nautical charts of the United States Navy. As fixed points were
taken the towns of La Coloma on the Southern coast and Santa Lucia,
Puerto Esperanza, Verracos, Puerto Blanco, Bahia Honda, Cabanas and
Mariel on the Northern coast. As the reader will see. La Coloma is not to
be found on our map. We knew, however, by pace-compass survey, the
relative position of the town of Pinar del Rio with regard to La Coloma.

We further had at our disposal a special map of the Carretera Central.
The direction of the road on this special map greatly differed from the
direction of this same road on the military map, e.g. the town of Santa
Cruz de los Pinos is situated about 12 km to the North on the latter. We
could check the directions of the Carretera Central at various places and
as our observations tallied more or less with the military map, we ignored
the special map of the highway.

the larger crystals are blueish pleochroitic (glaucophane). Albite is constantly
found in large and smaller quantities. It is developed as very clear allotrio-
morphic poikihtic crystals. Also zoisite is always found, often in large
quantities and in well developed crystals. Garnet is common in most of
the amphibolitic rocks. Large, idiomorphic crystals are found in the glau-
cophane bearing rocks, e.g. loc. A. 773, North of San Cristobal. Muscovite
crystals are accessory in most rocks. At loc. V. 726, North East of La Palma,
however, large muscovite scales are numerous. Chlorite, titanite and ore
are found as accessory minerals. The texture of the rocks is predominantly
irregular and without linear arrangement of the minerals, with the excep-
tion of a rock found at loc. L. 877, South of La Palma, which shows
linear structure. Other localities, where strongly metamorphic amphibolitic
rocks were found, are: loc. A. 698, North East of San Cristobal, on the
trail to Rosario, loc. M. 1053, South of Bahia Honda and loc. V. 818, near
Saroa, which is situated North East of Candelaria.

The greater part of the amphibole plagioclase rocks occur in
the Serpentine strip, which can be continued in East West direction South
of Bahia Honda. Locs. in this vicinity, where these rocks were sampled,
are Loc. M. 1041, M. 1068, M. 1069 and M. 1080. Another findspot of this
kind of rock is loc. L. 905, North West of the town of Santa Cruz de los
Pinos. The rocks always occur in the Serpentine regions, and we consider
them to be inclusions, though geological evidence supporting this suppo-
sition is wanting. It is for instance also possible that dikes in the Serpentine
have been altered under the influence of tcctonical stresses into these horn-
blende plagioclase rocks.

Thin-sections of these rocks consist of allotriomorphic green and
brownish-green, pleochroitic hornblende and an equal quantity of allo-
triomorphic, polluted plagioclase of andcsine-labradorite composition. In
cases, the plagioclase crystals are twinned and often they are sericitized.
Linear structure occurs, e.g. at loc. M. 1068.

Gabbroid dikes: M. G. Rutten (64) mentions the occurrence of
gabbroid dikes in the Serpentine areas in the Northern Santa Clara province.
He draws the conclusion that the intrusion must have taken place before
or during the orogenetic phase following the sedimentation of the Maes-
trichtian Habana beds, as the intrusions are only found in the Serpentine
displaced by this orogcnctic activity and not in the nearby situated other
formations.

In four placcs gabbroid rocks were sampled in the province of Pinar del
Rio. At Iocs. A. 731 and A. 733, South West of Cabanas, medium grained
green and white specklcd rocks consisting under the microscope of large
twinned plagioclasc of basic composition (labradorite), partly sericitized,
and of diallage and rhombic pyroxene. Olivine is found in large quantities'
and is partly serpentinized. Magnetite occurs as small crystals A rock
sampled at loc. V. 890, North East of La Palma is more altered. The diallage

is partly uralitized, the plagioclase is andesine. Olivine and ore are lacking.
A rock, found at loc. L. 946, North of Guanajay, agrees with those found
at loc. A. 733. It contains numerous olivine crystals.

All the above mentioned findspots occur in the Serpentine or at its
boundary, thus supporting Rutten's statement. An exception is loc. M. 1034,
South of Bahia Honda, where a gabbroid dike occurs in the Tuff Series.
Near to this loc. about 150 m to the South, however. Serpentine is found
at loc. M. 1036. In the area between those two findspots tuffaceous porphy-
rites were noted but not sampled. Exact evidence is consequently wanting,
and we may not draw any conclusions.

A rock, collected at the boundary of a Serpentine outcrop (loc. M. 1039,
South of Bahia Honda) is a gabbro-diabase. A thin-section shows clear,
well twinned lath shaped plagioclasc. The composition is basic, varying
from labradorite to bytownite. The texture is coarsely ophitic. The
monocline pyroxene crystals are allotriomorphic and partly uralitized.

At two localities in the province of Pinar del Rio we found rocks allied
to a dioritical magma. We shall procccd to describe the localities and the
rocks separately.

Locality H. 985 is situated between Guane and La Sierra at the
Eastern side of the road connecting both places. We drew a small sketch
map on which the situation of the outcrops of the adjacent rocks arc
indicated (fig. 1).

The dioritic rock (d
on the map) is light grayish
white of colour and coarsc
grained. Under the micro-
scope the rock consists of
strongly allotriomorphic
quartz with cloudy extinc-
tion and of plagioclasc,
found in smaller quantities
than the quartz, of an
acid composition (albite)
and dearly twinned. The
lamcls are bent, owing to

To the West of this outcrop, limcstonc-brccc.as were noted (L bi^O.
but not sampled. This limcstonc-brcccia might be an outcrop or^ i-iarana
formation of Mountain facies. To the Hast of the outcrop °fnbsp;^^

.mestones (L on the map), which are also found Lu h » h'Set«
TnThnbsp;rt resemble the limestones found ntercalated

to occur as a large boulder in this formation m^fnto tonsid^rS
he large size of the outcrop, which is several metres, 4 prefer to con^der
.t as a leucocratic vein of the diorite magma, breaking tLougM^ ll

The other findspot of dioritic rock is situated North West of Bahia
Honda at loc. V. 85 i. Nearby, to the North of this outcrop we find SeSet
tine exposed whereas to the South tuffaceous rocks were noteZnd
sampled. The dioritic rock is a strongly crushed diorite-pegmatite consisting

Fragments strongly resembling this rock are found frequLly in the I^rana
formation At the same locality we sampled a malchitic rock, of pandto
triomorphic texture, consisting of basic plagioclase and partirchSted
amphibole and quartz. Zoisite and sphene L also found We takequot; oth
rocks found at tins locality to be directly connected with the dioritic magma

The age of the rocks at both localities is difficult to establish As the
—dings of loc. H. 985 are badly exposed and, moreover of a ot
plicated nature, we will only consider loc. V, 851. The dioritic vein at Z
ocahty cuts through the Tuff Series and may be considered younger than
±ese strata. However, signs of contact-metamorphism were no? fo^nd
On account of the numerous fragments of dioritic rock found in the Habana

mentation of these beds, i e. before Upper Cretaceous (Maestrichtian)
times. The age of the intrusion of dioritic rock in Pinar del Rio province
^rees well with the age of the diorites found in Northern Santa Clara by
M. G. Rutten (64) and in Southern Santa Clara by A. Thiadens. (74)

The name Habana formation was used by Palmer (59) for Uoner
Cretaceous beds in the vicinity of the town of Habana, M. G. Rutten «4)
applies the name Habana formation for beds of the same age exposed in
Northern S^ta Clara carrying a fauna idemical with the fossils found
m the neighbourhood of Habana, but differing petrographically and
hthologically. On account of the existence of practically the same fauna
m the strata exposed in Planar del Rio province, we also use the name
Habana formation for these beds.

The Habana formation exposed in Pinar del Rio can be divided in
two different groups of rocks, representing two sharply contrasting facies.
One facies, which we called quot;Mountain faciesquot;, occurs in the mountain
regions; its rocks have been wedged into the older rocks of the Tuff Series
and of the San Andres formation. The other facies, called '^Eastern facies
occurs in the sediment belt around the mountain region. These beds can
only be separated from the Upper Eocene and Ohgocene strata by paleonto-
logical evidence.

The position of the beds of Eastern facies seems to point to a younger
age than that of the beds of Mountain facies found at the overthrusts in
the San Andres formation and Tuff Series. The Upper Cretaceous-Lower
Terdary complex seems to be sedimentated against or upon the mountain
complex. Difference of tectonic style in the two regions, together with the
post-miocene faulting which fixed the recent shape of the mountains cause
this impression. Both strata. Mountain facies and Eastern facies, however,
carry the same Forammfera, e.g. Vaughanina, Orhtoides bromi, Lepid-
orbitoides, Omphalocyclus, Torreina and Camerina sp., indicating the same age.

Numerous well preserved Rudists were found in the Habana formation
of Eastern facies, whereas in the beds of Mountain facies only fragments
of Rudists are found. The possibility that these fragments are secondary
deposits in younger strata is rejected by us on account of the presence
of the same Foraminifera in both deposits (fig. 2).

Age of the Habana formation: On account of the occurting
Foraminifera, especially the genera Orbitoides, Omphalocyclus and Lepidorbi-
toides, we reckon the Habana formation to be of Upper Cretaceous age,
corresponding with the Maesttichtian of Europe. At two Rudist-findspots,
loc. L. 818, North-West of the town of Pinar del Rio and loc. M. 940,
North-West of Tranca, Orbitoids, e.g. Orbitoides bronmi were found, conse-
quendy we assume the Rudists beds to be of Macstrichtian age.

coarse conglomerates of Upper CreTaTeous or III. P
dioritic material in rocks SF und^b dly 'VbTa aSquot; Thlf'
rocks of both facies, e.g. at iocs. M. loJs aTl^.O®« ' South o?Blhk
Honda loc A. 754, South East of Mariel, ioc. V. 843 North We« nf
Bahia Honda and at loc. H. 923, South fiit of Las PozaT PartkH

Tertiary strata^For this reason, the formaLfZl^tenTe s r^e cZT.
on the .nap. Only those places, where paleontologifal ev dence^ndica°e
the exact age, were coloured red in case of the occurrencT nfTw
Cretaceous beds, whereas a special signature indicates LdsTuLr Eocene
or Oligocene age. A detailed survey will brintr out wWW fi! uquot;
chalks and marls and calcareous sandLnes oc^^n^^nlt gt m^st
be reckoned to belong to the Upper Cretaceous or Lower TeXy stmf
We realise that the combim;ng of Upper Cretaceous and Lower TertTary
on the map is far from satisfactory, the more so as a stratigraphical unco7
formity exists and a tectonical disconformity between the Upper Cretaceous
and the Upper Eocene may be expected in analogy with ^tegeSogy S
the Santa Clara province (64). Evidence of this angular unconformit®/ha
not been found by us in the Pinar del Rio province

The localities, where rocks of the Habana formation of Eastern facies
are found, are given ,n table on page 23, together with the oXw
F„ra,«,«,fira, Rudists and Rudists fragments, thich established the ale
The Forammijera, however, occur for the greater part in thin-sections nf
rocks; thus reliable and typical sections were not'^always obtSed The
mutual association ol Poramimfera or the association of them with Rudists
or Rudist fragments ascertain sufficiently, in our opinion, the age of the
inH . ; head quot;Orbitoidsquot; were put downnbsp;howing

indistinct affinities to Upper Cretaceous genera. Their state of priservation
IS often very bad on account of recrystallization. This recrystallization is
not found in specimens of Upper Eocene age. The small C^»™ show
attimties to Camerma dtcktrscm described by Mrs. D. Palmer (57) from the
Upper Cretaceous beds in the Habana province.

For those, interested in well preserved R^^ists, we draw the attent^^^
to the Iocs. A. 645, A. 647, H. 774, H. 787, H. 802, H. H;961 L. 818
M. 938, M. 940, M. 966, V. 614, V. 843a. The material collected by us at
these localities has already been described by the author in a paper, accepted
for publication by the Journal of Paleontology.

Description of rocks of Habana formation Eastern facies:
The rocks are for the greater part fine conglomerates or congl°^
calcareous sandstones. They are white to gray in colour, in contradistinct^n
with the rocks of Mountain facies, which are dark grayish-blue. They
carry a large amount of calcareous matrix. The constituents of the rocks
are clear rounded or angular quartz, well-lamellated and non-lamellated
pagioc^^^^^^^^ of a basic composition (labradorite). The size of the quartz and
felfpars varies in differen? rocks from small to large Rounded porphyrite
fragments are always present, in cases even form the mam constituent
Th! porphyrites consist of smaller or larger basic plagioclase phenocrysts
in a vitric groundmass, often coloured red by iron infiltration. In cases,
when the matrix is more crystalline, it consists of small plagioclase laths
and small magnetite ore grains. We mentioned already the occurrence of
detritical diorite fragments. Occasionally we find roundednbsp;f

phyllitic and quartzitic rock, cleariy derived from the San Andres formation
rLe constituents dominate in a rock found at loc. L 930 Nor^ of he
town of Cayajabos. Chert fragments, amphibole crystals and zoisite grains

ApTr^from the conglomerates and the calcareous sandstones we find
white to gray limestones or sandy limestones, from which the Rudists
may originate ; they have been principally collected out of loose soil, more

Mountain facies of the Habana formation: Rocks of Upper
Cretaceous age (Maestrichtian of Europe) are found wedged into the ban
Andres formation and the Tuff Series. Exposures of these rocks are found
at the foot of many typical quot;Mogotesquot; in the Western part of the Organos
mountains throwing a new light on the tectonics of this region. Each
outcrop, often accompanied by Serpentine, points to an anomalous
contact with the older formarions. We found them numerously in the
Eastern part of the Organos mountains and also in the small area North
of Guanajay, were the beds occur partly as steep infoldings.

The rocks of Mountain facies of the Habana formation are, in the
field in many cases difficult to disringuish from the limestones of San
Andres formation or Tuff Series. Only the coarser conglomerates or
breccias were recognized in the field as Upper Cretaceous strata, because
of the Rudists fragments often macroscopically visible. Thm-sections of

Upper Cretaceous Habana roclfs We menSt th ^
a part of the outcrops of rocks of Mo f rnbsp;'hat

With respect to the fauna found in the rock of ^^ . ■ r ■
same considerations we made with resard to r. fnbsp;facies, the

facies, hold true: consequently, we rrfer to them Th'
respective faunas are given in'the tabk on paTe 23

acid to basic plagioclase as -in col^tue^quot; C^^uL^ p^'rp^^^^^^^^^^^^^
fragments are in the minority. The difference with fh^Voinbsp;diorite

amount of quart, and the impure matrix ;?he difference Sthe^ocrof
the Tuff Series is the occurrence of quartz and of dioritir ^
^terminably smallnbsp;occur!t Ifrquot;gr eter-quot;

minatlon on paleontologlcal data was impossible. On account of the
occurrence of dioritic material we favour an Upper Cretaceous age of L
beds. The other possibility, that the strata are younger and paft of tL
Upper Eocene, does not seem probable, as we never found evidence of
Wne beds wedged in with the Upper Cretaceous layers in the mountahi

The beds are found, e.g. North of La Palma at loc. L. 874 The sreenisb
sandy rock consists chieffy of twinned plagioclase felspar, of albiteoligo-

clase composition, rounded and splintered quartz crystals, rounded
porphyrite fragments, dioritic material, chert fragments, greemsh brown
pleochroitic biotite and muscovite plates. The matrix is a mixture of
chlorite-limonite and calcite. Rocks which principally resemble the above
described rock are found at loc. M. 949, North East of Vinales, loc. M. 919,
North East of Sumidero, loc. M.914, South West of Sumidero, together
with a limestone breccia, carrying small Camerinas showing a ffimties with
Camerina dickersoni (Upper Cretaceous), loc. L. 1053, East of San Vicente,
together with a limestone breccia in which Orbitoides W«. was found
loc. M.958, North of San Diego de lós Banos and at loc. V. 950, East
of Guane. All locahties mentioned above are situated m the Western part
of the Organos mountains (quot;Mogotequot; regions).

Coarse conglomerates are a typical feature in the Upper Cretaceous-
Lower Tertiary strata running from San Juan y Martinez to San Diego de
los Banos. We shall discuss the constituents of the conglomerates more

^quot;quot;^^^bne of the richest findspots of pebbles of different nature is loc. A. 608,
West of the town of Pinar del Rio, where several samples were coHected.
Numerous are porphyritic or diabase rocks, the greater part of them
strongly weathered and altered. Some of the porphyrites are silicified, and
only the two generations of plagioclase felspars can be recogmzed. The
diabases show an ophitic texture, the augites are for the greater part
uralitized, the plagioclase felspars are of an acid composition (oligoclase)
ore in the form of ilmenite is common, accessory minerals are apatite and
sphene. Quartz is often found as a rest-crystallization. The above described
rocks are clearly allied to the rocks of the Tuff Series. Rocks deriving from
a dioritic magma are also found at loc. A. 608, e.g. an albitite, constisting
of polluted plagioclase felspars often granophyriccally intergrown with
quartz. Accessory minerals are sphene and epidote and ore. A pebble of
malchitic rock consists of twinned plagioclase felspars of a basic com-
position (andesine-labradorite), clear, strongly allotriomorphic quartz and
amphibole. The amphibole crystals are blueish-green pleochroitic and
idiomorphic. Accessory minerals are sphene, apatite and magnetite. Blue
and violet limestone pebbles occur, probably derived from the San Andres
formation; also a white limestone, carrying corals and Lithothamnium.
One pebble contains a badly preserved Orbitoid, pointing to a post-Upper
Cretaceous age of the conglomerate at least.

At loc. L. 849, North East of San Diego de los Banos, porphyritic
and dioritic pebbles are found. One rock is a diorite-aplite, consisting or
allotriomorphic quartz and plagioclase crystals. The plagioclases are
sometimes twinned and of an acid composition; they are partly sericitized
and contain quartz globules. Some muscovite plates occur, and a few large

South West of San Diego de los Bafios at lol H 79 a Zrite ne.
matite pebble was collected. The structure is coarse c«,?, 11
constituents are large, idiomorphic, polluted, twinneTalbTe c^
granophy„ca% intergrown plagioclase and quart.. Ace sor^ mte^ls
are sphene, chlorite and ilmenite. The findspot of this pebble i^ n the
Eocene area on the map. Paleontological evidence establishing the È^L

North East of the Organos mountains, consist of white limestones
conglomerates, cakareous sandstones, marls and chalks. We alreadv

The Upper Eocene age of the beds was established by the occurrence
fvinbsp;of the genera Dictjoconus, Camerina, Lepidocjclina

Hehcoleptdtna ^nA DiscocjcUna. The Foraminifera occur in different kinds
of rock. At loc. L. 829 they are found in calcareous sandstones, tog thS
with fragments of Rudists, which dearly are a secondary deposit A^s one
is indined to attribute a Macstrichtian age to those strata were Rudist
fragments are found, this occurrence in the Upper Eocene beds proves
hat careful cxammation for other paleontological data is required. At
loc. L. 831 Foramimfera of the genera Dictjoconus, Camerina, LepidocycUna
and Disc^jcUna -^^t^ioun^ in a coarse conglomerate, containing porphyrites
and pebbles of grayish blue limestones and cherts, derived from the San
Andres formation. Rounded fragments of Rudists also occur. Around the
town of Guanajay the Upper Eocene Foraminifera are found in white marls
and white limestones (Locs. M. 1029 and H.971). At loc. V. 804 North
East of Cayajabos, some rocks were sampled, which were derived from
an unknown depth out of an asphalt mine. The conglomeratic rock carries
Omphalocjclus (Macstrichtian) and badly preserved DiscocycUnae. Either
the Omphalocjcks is a secondary deposit or the DiscocJcUnae\^^^^z2.t already
in the Macstrichtian. Nearby, at loc. V. 802, we find rocks carrying Rudist

^^quot;^Apart from the larger Foraminijera, numerous smaller Foraminijera
e.g. Miliolidae, Globigerinidae, Carpenterias etc. occur. As they are found
principally in thin-sections of hmestones, no specific determination was

recent pubhcation Cushman and Bermudez (26) describe several
smaller Foraminijera of Upper Eocene age, which were coUected about
4.5 km. North of Guanajay on the road to Mariel. These Foraminijera belong
to the genera Bolivina, Virgulina and the hew genera Rectoeponides, Stichocibi-
cides and Neocarpenteria. In a second publication the same authors (27)
treat some new species of the genera CjchhcuUna, Siphonina and Crihro-
globorotalia. They were collected at Bermudez station 337 A., which is the
same locahty where the material studied in the former pubhcation was
derived from. However, the situation of this findspot is ^ow said to
be found in the last paper 4.5 km West of Guanajay instead of to the
North. On account of this controversy we did not mark these Eocene

Echinids, collected at a locality situated on the road from San Diego de
los Banos to the Carretera Central. We do not agree to his statement that
Middle Eocene might occur along this same road, as we have no paleonto-
logical evidence supporting this.nbsp;, • r^r

cene orogenesis. Evidence of a structural unconformity between the Upper
Cretaceous and the Upper Eocene was not found m Pinar del Rio.

Paleontological data estabhshing the Oligocene age of layers were
only found by us at a few localities. The marls, white hmestones and
sandstones show a great resemblance with the Upper Eocene strata. The
Oligocene beds carry larger Foraminijera of the sub-genera Nephrolepidina
and Eulepidina. At loc. M. 1027, West of Guanajay, Ohgocene sandstones,
carrying Lepidocjclina javosa lay concordant upon white hmestones and
marls of Upper Eocenc age. In two localities, North of Guanajay at loc.
L. 941 and North of Candelaria at locs. V. 782 and V. 783, white hmestones
carry Lepidocjclina of an eulepidine type. On account of the occurence of
these Foraminijera in limestones, the more or less accidental thm-sections
through them did not show clear characters of the fossils to justify a
specific determination. We did, however, get the impression that Lepido-
cjclina javosa occurs, on which fact the Oligocene age of the limestone
beds is based. Hadly (37) describes numerous smaller Foraminijera collected
by Mr. Norman E. Weisbord, 50 m South East of the entrance gate
to the Cuban Naval Academy at Mariel. The Foraminijera have been

of less than , 0 degrees'The dips ar! di^LdTr ou ht th:\tth1S
regions e.g. between Consolacion del Sur and Santa CruJ 1
to the North in the Northern parts e.g. Norfh of Ln^l How' ' =
observations in the Northern part are Icarse fh.r.f however, our
mainly founded on facts collect in the Sou^X^s quot;quot;quot;quot;quot;quot; quot;

In large areas, which are reckoned by us to the Oligomiocene outcrons
are scarce. The typical cavernous limestones only rafely outcrrfem'a
ted soil, often covered with quot;perdigonesquot;, the local nLe for hmo^tic
iron concretions. Sometimes we find coarse conglomerates cTskti^
mainly of quartzite and phyllite pebbles, derived from the San AndS
formation. We have no evidence which establishes the age of thesfCs
however, we assume an Oligomiocene age but they may be younlr '

Oligomiocene rocks consists of ForamWera
Gastropoda, Lamlhbranchiata, Echinidae and Antho^^oa. Especily ^e

Echinidae were sufficiently preserved for determination. This was done by
Mr J van SoEST, at the laboratory of the Utrecht University. The species
Clytea^ter lanceolatus was discerned. A full description of this species is given
in the paleontological part of this paper. Moulds and casts oi Gastropoda
are abundant in the limestone beds. A determination of the Lamellihranchiata
and the Corals was not made as the age of the beds is sufficiently estabhshed
by the Foraminifera and the Echinidae.

Age of the Oligomiocene beds: The Guinness limestones are
reckoned by Palmer (59), who gives a -summary of the former opinions
on the age of these beds, to be a quot;transitional phase between the Upper
Oligocene and the Lower Miocene.quot; He mentions the presence of Lepido-
cycUna and Miogypsina in the Guinness limestones. With regard to the latter,
we fully agree with Palmer. Miogypsina, together with Amphisorus matleyi
and Archaias are typical for the horizontal or slightly dipping Oligomiocene
strata. Amphisorus matleji from the Miocene beds in Jamaica has been
described by Vaughan (80). LepidocycUna, however, was not found by us
associated with Miogypsina or Amphisorus matleyi. LepidocycUna occurs,
so far as we know, in Pinar del Rio, only in the steeply folded strata,
underlying unconformably the Oligomiocene beds. Clypeaster lanceolatus
has been described by Cotteau (22) from the Miocene beds of Matanzas,
w hereas Lambert (42) reports the occurrence in the Miocene of Antigua.
In Jackson's opinion (41), who studied material from Panama and from
the vicinity of the town of Plabana, it should be an Oligocene species.
At the findspot of Clypeaster lanceolatus in Pinar del Rio, loc. V. 774,
North East of San Cristobal, we noted the occurrence of fossils charac-
teristic for the slightly folded OHgomiocene beds, e.g. moulds and casts
of Gastropoda, Lamellihranchiata and Amphisorus matleyi.

Contrary to former opinions, already mentioned in this oaoer in the
nh^rn San Andres formation,Ve consider firsforo^^^^^^^^^
phase to have occurred after the sedimentation of the Tuff Series Sfen
the Lower Cretaceous and Upper Cretaceous time. The a4 of \he w
antidme, which was the result of this orogenetic activity and of whU L
Soi^hern flank is exposed only in the Western part of Pinar dd Rb runs

East direction turning to North North West - East South East in the
neighbourhood and North of San Diego de los Banos

Hd It iT^'^^u^ the limestone hills in this Western part of Pinar
dd Rio follows the same directions, accentuating the general strike and
supporting our opinion that the quot;Mogotesquot; are intlcalatfd in the quartSe
phylli^^e beds. If the limestones covered unconformably an already Irongly
folded quartzite phyllite complex it would be highly improbable tLt owing
to a later orogenesis, the strike of the limestones beds would run iS
practically the same direction as the strike of the quartzite phyllite beds
A few deviations of the Northern dip of the Northern wing of the
antidine are found. This is for instance the case North West of Sumidero
where we found several Southern dips and one well developed, small
local antidme at loc. V. 567. The latter was dearly overturned to the
South East. Horizontal hmestones, only slightly dipping to the East and
West in p aces and in no way differing from the ordinary hmestones
intercalated in the quartzite phyllite beds of the San Andres formation
were found along the road from Guane to La Sierra at loc. H 980

In the Eastern part of the Organos mountains the strikes of the San
Andr^ formation and the Tuff Series runs rather irregularly, more or less
in a West to East direction. The younger parts of the Northern flank of
the antichne are exposed in this region (Tuff Series), while a small secon-
dary antichne is devdoped North of Bahia Honda, where tuffaceous rocks
are again exposed. The Tuff Series runs into the sea between La Mulata
and Verracos.

At the Southern boundary of the Eastern part of the San Andres
formation we found occasionally Southern dips. It is possible, that the
antidinal axis found in the Western part, may be continued alone the
above mentioned Southern boundary.

East of the Organos mountains the older structures are covered by
the Upper Cretaceous and Lower Tertiary strata. The older structures
rise to the surface again between the towns of Mariel and Guanajay where

they appear to be folded in detail with irregular Southern, vertical, and
Northern dips.

A second orogenetic phase may have taken place after the sedimen-
tation of the Habana formation upon the partially eroded older structures
and before the sedimentation of the Lower Tertiary.

After the sedimentation of part of the Ohgocene conformably upon
the Upper Eocene in the regions around the mountain district a new
inter-Oligocene orogenesis occurred. The direction of the strikes of the
Upper Eocene and Oligocene beds in the Eastern part of Pinar del Rio,
runs generally from West to East, but is-also often irregular. On the whole,

The Upper Cretaceous and the Lower Tertiary, exposed South ot the
boundary of the San Andres formation, show strikes running more or
less parallel with the strikes in the San Andres formation. The fact, that
the general trend of the second and third orogenesis runs parallel to that
of the first, weakens our supposition, made in the beginning of this chapter,
that we could expect a different trend in the limestones to that in the quartzite
phyllite formation, if an angular disconformity between the two should be
found. When, however, hmestone beds with a certain strike are present m
the underground, we may expect an influence, even a dominating influence,
of this resistant structures upon the trends of the later orogenesis. We
refer to the neighbourhood of San Diego de los Banos, where the Upper
Eocene layers exposed along the road to the Carretera Central, show the
same directions of the strike as the San Andres formation (Loma La Guira).
The different Rudists findspots, nearby, which may be expected to occur
in one level, show a direction crossing the direction of the strikes of the
Upper Eocene and San Andres formation. If the findspots of the Rudists,
collected out of loose soil, may be reckoned to mark more or less the strike
of the Rudists beds (Habana formation), we should have at this place an
indication . of an angular disconformity between the Habana formation

In the Southern band of transgressive formations we find generally
a Southern dip, with one exception: North East of Consolacion del Sur,
where in the core of an anticline the Habana formation outcrops.

In the mountain regions we find the Habana formation of Mountain
facies wedged into the San Andres formation and into the Tuff Series. The
position of the limestone breccias (Habana formation) at the foot of the
quot;Mogotesquot; and in the valleys cut through the limestone hills, clearly points
to an anomalous contact with the older formations. In the region of the
San Andres formation the beds of the Habana formation are often found
accompanied by Serpentine. We suggest, that along the soft and smooth
surface of the Serpentine rock, overthrusting took place.

From the regions surrounding the mountains we have evidence of
an inter-oligocene orogenesis. In the Northern Santa Clara province (64)
and in the Southern Santa Clara province (74) we have evidence of an

orogenetic phase between the Upper Cretaceous and the Upper Eocene
mther the latter or the inter-oligocene orogenesis caused the overthrusting
(wedging) in Pinar del Rio. With regard to the nature of the overthrusting
It appears to be superficial. The beds of the Tuff Series and the beds of t£
San Andres formation were not displaced with regard to each other At
the anomalous contacts, in the San Andres formation, no rocks of the
Tuff Series are found. Even near the boundary between the formations
no evidence of an anomalous contact between the San Andres formation
and the Tuff Series has been found. The occurrence of rocks of the San
Andres formation in the Tuff Series is, however, difficult to ascertain as
the hmestones and cherts, the principal elements of the San Andres
formation in these parts, are not to be distinguished from the same beds
occurring in the Tuff Series. However, rocks of Cayetano facies, typical
elements of the San Andres formation have never been found near the
anomalous contacts in the Tuff Series.

In some regions of the San Andres formation we find a gentler type
of orogenesis. Instead of overthrusts we find the beds of Habana formation
of Mountain facies exposed in the synclines. This is for instance the case
North of the town of La Palma and in the strata exposed North of Guanajay
which are also reckoned by us to the San Andres formation. The tectonic
style of the latter parts resembles the tectonic style found in the regions
where the beds of Habana formation of Eastern facies are exposed.

In the greater part of the outcrops of Habana formation of Mountain
facies, no strike or dip could be measured. Only in a few localities, did we
feel justified to connect some nearby outcrops. However, the outcrops
seem to occur in bands running parallel to the limestone hills in the Western
part and also parallel to the strike of the San Andres formation and Tuff
Series in the Eastern part. The former is demonstrated along the Northern
boundary of the Sierra Ancon, West of San Vicente, where in all probability
three outcrops of Habana formation of Mountain facies may be connected
with each other. If this holds true, we see that, as in the younger sediment
belt around the mountains, the trend of the pre-maestrichtian orogenesis
runs parallel to that of the post-maestrichtian, orogenetic phase.

The fourth and last orogenetic phase occurred after the deposition
of the Oligomiocene beds. This orogenetic phase, however, is not to be
compared with the former ones, which were much stronger. The maximum
dip of the Oligomiocene beds is 10 degrees, while often they are found in
horizontal position.

Post-Miocene faulting fixed the Southern boundary and the recent
shape of the Organos mountains. We based the presence of this fault chiefly
on morphologic arguments.

As the larger structures are clearly shown on our geological map, we
did not draw any sections. Of the detailed structures, we have insufficient
data to compose sections, that would approach reality, so we prefer to
leave them out.

Parts of the fossils collected by us in the province of Pinar del Rio
have been or will be descnbed in other papers in order to make the results
more accessible to those interested chiefly in paleontological matters. The
faunal lists with the findspots given in a previous chapter and m a paper
already published, are copied in this chapter, in order to give a complete

The Ammonites, also collected from the San Andres formation will
be specifically determined by Prof. Jaworski, who will pubhsh the results
of his study in due course. His preliminary investigation fixed the age of
the different parts of the San Andres formadon.

Some well preserved Echinids were studied by Mr. J. van Soest. The
description of them is published in this paper.

The Larger Foraminijera, collected out of the Habana formation. Upper
Eocene and Oligocene were specifically determined by the author ; the

Faunal lists: We shall first give a list of the fossils, the occurrence
of which is not confined to a special formation.

Glohiserinidae at localities: A. 606, A. 711, H. 820, H. 897, H. 898,
H.970, H.973, FL 975, L. 924, L. 935, L. 938, L. 940, L. 994, L. 999,
L. 1000, M. 1038, V. 790, V. 804.

Miliolidae at localities : A. 600, A. 604, A. 621, A. 623, A. 626, A. 684,
A. 685, A. 721, A. 726, A. 730, A. 737, H.801, H. 832, H. 873, H. 880,
H.893, H.895, H. 896, H. 898, H. 923, H.970, L. 757, L.761, L. 832,
L.835 L.836, L. 838, L. 840, L.841, L.913, L. 926, L. 997, M. 905,
M.927, M. 1009, V. 696, V. 699, V.781, V. 795, V. 804, V. 826, V. 843,
V.919.

Lamellaptjchus angulocostatus (Pet.) ƒ. typenbsp;V. 826, V. 868.
Lamellaptjchus angulocostatus (Pet.) var.

Orhitoides apiculata (Schlumb.)
Orhitoides hronmi (Ellis)

Omphalocjclus ?nacropora Bronn
Omphalocjclus sp.
Torreina sp.
Lepidorhitoides sp.

Orhignja mullerriedi Vermunt
Orhignja sp.

Vaccinites macgjllavrji Palmer
Vaccinites sp.

Pironea cf. peruviana Gerth
Barrettia sparcilirata Whitfield
Barrettia monilifera Woodward
Barrettia multilirata Whitfield
Parastroma cf. quitarti Palmer

A. 730, A. 754, A. 773 ?, H. 822,
L.955, L.983, L. 985, L. 1003 ?,
M. 1009, M. 1021, M. 1038,
M. 1049 ?, M. 1057, M. 1065,
V. 699, V. 795, V. 804, V. 826 ^^
V.841, V.843 ?, V.875, V.88l!
A. 677, A. 678, A. 754, H. 774,
H.954, L.817, L.949, L.955,
L. 983, L. 985, L. 1003, M.914,
M. 938, M. 1021, M. 1038, M. 1065,
V. 826.

A. 673, A. 677 ?, A 678, A. 684,
A.685, A.773, H.822, H. 823,
H.832, H.880, H. 893, H. 898,
L.887, L. 930, L. 1003, L. 1013,
M. 1009, M. 1038, V. 843, V. 875,
V. 881.
M. 940.

L.955, L. 1013, V. 795, V. 804.
A.773, L. 930, V. 802.
A. 730, A. 754, L.955, L. 985,
M. 1021, M. 1057 ?, M. 1062 ?,
M. 1065, V. 699, V. 804, V.841,
V.875.
L. 818.
H. 774.

Torreites sanche^i (Douvillé)
Radiolites macroplicatm Whitfield i)
Biradiolites cubensis Douvillé
Biradiolites cf. aquitanicus Toucas
Biradiolites tschoppi Vermunt
Biradiolites macgillavryi Vermunt
Biradiolites sp.
Biradiolites sp.

Tampsia rutteni Vermunt
Chiapasella pauciplicata Müllerried
Chiapasella cubensis Rutten
Chiapasella sp.

A. 674, A.678, A. 740, H. 788,
H. 823, H. 832, H. 893, H. 904,
H. 906, H. 923, H. 927, H. 928,
H. 954, L. 949, L. 955, L.957,
L.973, L.983, L. 985, L. 1003,
L. 1013, M. 937, M. 968, M. 1009,
M. 1032, M. 1046, M. 1049,
M. 1057, M. 1062, M. 1073,
M. 1077, V.698, V. 795, V. 802,
V.804, V.820, V.826, V.841,
V.843, V.875, V.881, V. 894.

Localities :
H.792, H. 841, L. 829, L.831,
V.536, V. 696.
L. 829, L.831, M. 1028.
M. 1028.

Operculina floridensis (Fleilprin) Cushman L. 831.
Heterostegina antillea Cushmannbsp;L. 831.

Camerina petri M. Rutten
Camerina malbertii M. Rutten
Camerina sp.

LepidocycUna mortoni Cushman
LepidocycUna mein'^^eri Vaughan
LepidocycUna marginata Michelotti
LepidocycUna piedrasensis Vaughan
LepidocycUna semmesi Vaughan and Cole
LepidocycUna sp.

HeUcolepidina spiraUs Tobler
DiscocycUna marginata Cushman
DiscocycUna cf. clarki Cushman
DiscocycUna sp.

Archaias sp.

Camerina sp.
Miogypsina sp.

A. 600, A. 620, A.621, A. 622
A. 623, A. 624, A. 626, A.712;
H.762, H.968, L. 757, L. 758,
L. 761, L.835, L. 836, L. 838,
L.840, L.841, L.913, L. 1008,
M. 905, M. 927, M. 968, M. 1007,
M. 1024, V. 776, V. 777, V. 780,
V.781, V.919.

A. 624, A. 711, H.762, L. 757,
L.761, L.835, L.840, L.841,
L. 1008, M. 905, M. 1007, V. 776,
V. 777, V. 780, V. 781.
V. 776, V. 777.

A.621, A. 623, A. 624, A. 626,
H.895, L.757, L.761, L. 838,
L.840, L.841, L. 1008, M. 905,
M. 1007, V.776, V.777, V. 780,
V.781.
V. 774.

Fossils:

Camerina petri M. Rutten ?
Camerina sp.

LepidocycUna piedrasensis Vaughan
LepidocycUna dilatata Michelotti
LepidocycUna favosa Cushman
LepidocycUna sp.

List of fossils

Fossils:
Amphisorus matleyi Vaughan

Systematic descriptions:
Genus Dictyoconus Blanckenhorn, 1900.
Dictyoconus sp.
Plate, figure 6.

mar^hial trough are divided into 2 to 4 cellules. The distance of the plat-
format the base is 160 ^ to 250 Diameter of the base, 2.4 mm to 3.6 mm
SI mm to 3 mm. The general appearance of the specimens resemble
Sat of Dictyoconus americams. However, the large distance between the
pWorms at'the base is more in agreement with Dutyoco^^^^^^^^

M. Ru™. 1935. Jour. Paleontology. Vol. 9. pp. 530. 531. pL 59. figs. 1-5. textfig. 2.

On the whole our specimens agree well with
Some slight differences occur e.g. one specimen consists of 9 whorls.
Lmber of septa in the last whorl 32. Diameter 7.1 mm thickne^ 2.7 mm
Another specimen though agreeing in outer measures ^ C ^ de^^^^^^^^^^
from the inner features, the chambers being higher than long ^^^ ^^^^^^^^^^^
resembling C malhertii. As only one specimen was found in ^he Oligocene
k mTy be^regarded as washed out of the Eocene strata. Diameter 3.8 mm

Camerina Malbertii M. Rutten.
M. Ru™. 1935. Jour. Paleontology. Vol. 9. pp. 531.532. pi. 60. figs. 8-10 ; textfig. 2.

Only one specimen was found, which is intermediate betw^n C. petri
and C malbertii by its outer measures. I reckon this form to C vm^ertn
for the shape of its chambers, which are higher than long. Diameter 8.3 mm,

thicknes^sj.^^mm^ Pinar del Rio, Cuba. Hypotype, Min. Geol. Inst., Univ.
Utrecht, D. 14592.

1) The D.-numbcrs refer to the collcction of slides in the Miner.-Gcol. Institute at Utrecht.

Involute, small, thick forms, found in shdes of Upper Cretaceous
hmestones of the Habana formation. Number of whorls is 3—4 They are
characterized by a conspicuous groove. Diameter 0.74 mm to 0 96 mm-
thickness 0.44 mm to 0.63 mm. In aU probability the specimens belong
to Camerina dickersoni. A recent study of Voorwijk (83) proves that there
exist transitional forms between material, agreeing weh with our specimens
and Camerina dickersoni.

Operculina floridensij Cushman, 1921, U.S. Geol. Survey, Prof. Paper 128-E., p. 130, pi. XX, fig. 12

Flat forms with a sometimes eccentric low umbo over the first whorls
Surface of this umbo ornamented with granules and costae. Septa strongly
curved backwards, especially in the last whorl. Chambers 5 times as high
as long. Number of whorls 2J to 31. No granules on the shghtly raised
sutures of the last whorl as with 0. vaughani. Diameter 3.3 mm to 7.7 mm,
thickness 0.90 mm, to 1.20 mm. Number of septa in the last whorl 22—3o!

Upper Eocene, Pinar del Rio, Cuba. Hypotypes, Min. Geol. Instquot;
Univ. Utrecht, D. 14593—14598.

Heterostegina antillea Cushman, 1921, U.S. Geol. Survey, Prof. Paper 128-e., p. 131, pi. xx. figs. 13, 14.

Flat forms with an eccentric umbo above the first whorls. Surface
papillate on the umbo and on the sutures. Diameter 8 mm, thickness 1.2 mm
to 1.5 mm. Number of whorls 2\ to 3.

This species is recorded from the Oligocene of the Island of Antigua
by Cushman (25). The occurrence of Heterostegina antillea in Pinar del Rio
together with typical Eocene Foraminifera, e.g. Dictyoconus, proves that
this species existed already in the Eocene.

Upper Eocene, Pinar del Rio, Cuba. Hypotypes, Min. Geol. Inst.
Univ. Utrecht, D. 14599—14600.

Genus Amphisorus Ehrenberg, 1840.
Amphisorus matleyi Vaughan
Plate, figures 1—3.
Amphisorus rgt;,atkyi Vaughn. 1929, Jour. Paleontology. Vol. 3, No. 4, pp. 380,381.382, pi. 41, figs. 1-4.

A common form in the Oligomiocene of Pinar del Rio. It agrees well
with Vaughan's description. Embryonal apparatus on transverse section
bicellular, measuring 440 ^ X 180 Horizontal section of eulepidine
type. The big chamber measures 555 the smaller one 260 The pores

Orbitoides apiculata Schlumbhkghr, 1901, Soc. Géol. France, 4quot; série, tome premier, pp. 465, 466, pi. VHI.
figs. 1, 4, 6, pi. IX, figs. 1, 4.

Surface badly preserved. In places, however coarsely reticulate
Embryonic chambers quadrilocular and embraced

test asymetrically developed, the flat side strongly fHled up with pillars
The layer of equatorial chambers is curved to the comcal side. This species
closely resembles O. bromh only O. apiculata is

6.8

5.7
7.2

3.8
5

Orbitoides palmeri described by Gravell (34) from Cuba, is smaller
(up to 4 mm) while its surface shows vermicular costae radiating from the

Gullowayina browni Ellis, 1932, Am. Mus. Novitates, No. 668, pp. 1-8, 9 figs, in text

As this form has already been sufficiently described only some outer
measures will be given :nbsp;^

4.1

Upper Cretaceous, Pinar del Rio, Cuba. Hypotypes, Min. Geol Inst
Univ. Utrecht, D. 14611—14627.nbsp;' '

Genus Lepidocyclina Gümbel, 1868.
Lepidocyclina (lepidocyclina) mortoni Cushman.

LepidocycUna mortoni Cushman, 1920, U.S. Geol. Survey, Prof. Paper 125-D., pp. 70 71 nl 27 figs 1-^
pi. 28, figs. I, 2.nbsp;' • . Ö • .

Lepidocyclina mortoni, Gravell and Hanna, 1935, Jour. Paleontology, Vol. 9, No. 4 pp 337 338 339
pi. 31, figs. 1-11, pi. 32, figs. 1-4.nbsp;....

Flat forms, sometimes with umbo. Surface papillate. Equatorial cham-
bers ogival, exceptionally becoming flat hexagonal and arranged on
intersecting curves. Diameter 4.8 mm to 6.8 mm, thickness 0.90 mm to
1.20 mm, embryonal apparatus 0.26 x 0.30 mm to 0.44 mm x 0.52 mm.

Upper Eocene, Pinar del Rio, Cuba. Hypotypes, Min. Geol. Inst.
Univ. Utrecht, D. 14654—14668.

Lepidocyclina dilatata, Lemoine and Douvillé, 1904, Mém. Soc. Géol. France, tome 12—2, pp. 12 13 pi I
fig. 2, pi. 2, figs. 8, 21, pi. 3, figs. 10, 15.

Large, flat undulate forms, sometimes with umbo. Surface finely
papillate. Embryonal apparatus of quot;eulepidinequot; type. Equatorial chambers

hexagonal and arranged on concentric circles. Pillars small and numerous
Diameter 7.5 mm to 11.7 mm, thickness 1.2 mm to 2.1 mm, embryonal

Thick lenticular forms. Surface papillate to coarse papillate. Pillars
disdnct. Equatorial chambers rhomboid to ogival and arranged on inter-
secting curves. The embryonic apparatus is too badly prese^ed for
determination. It resembles L. pustulosa, is, however, larger. Diameter

Upper Eocene, Pinar del Rio, Cuba. Hypotypes, Mm. Geol. Inst.,
Univ. Utrecht, D. 14734—14743.

Lepidocyclina [Helicolepidina) spiralis, Toblek. 1922, Eclogae geol. Hclv.. Vol. 17 No. 3' PP-nbsp;„

Helicolepidina spiralis, Bakkek. 1934, Jour. Paleontology, Vol. 8, No. 3. pp. 345,346, textfigs. la. Ic, pi. 47,

Only two specimens were found, both megalosphedcal. Surface of
the test is coarsely polygonal with small papillae. No flange Internal struc-
ture agrees with Tobler's description. Diameter 5 mm and 5 3 mm thickness
1.8 mm and 2.4 mm. Diameter of initial embryomc chamber 150 /x.

Upper Eocene, Pinar del Rio, Cuba. Hypotypes, Mm. Geol. Inst.,
Univ. Utrecht, D. 14752—14753.

Genus Discocyclina Giimbel, 1868.
Discocyclina (Discocyclina) marginata (Cushman).
Plate, figures 7, 8.
Orthophrag^ina .,argiua,a, Cushman, 1919, Carnegie Inst. Wash. Pub. 291, p. 56, pi. 1, fig. 2, pi. 2, fig. 4.

Thick lenticular forms with a broad flange, which is thickened near
the periphery. Surface is smooth but the distal end of the pillars is distinct
pardy by the different colouring, giving a papillate appearance. The radia
diameter of the equatorial chambers is three times larger than the tangential
and measures about 65 f. near the periphery. Lateral chambers very small.
Pillars are distinct, especially in the central region ; measunng 75 ^ to 110

Embryonal apparatus : one big chamber encircling a smaU one. The bigger
one measures 0.41 mm to 0.59 mm. Diameter 5.4 mm to 9.3 mm, thickness
z./ mm to 3.6 mm.

Orthophragmina clarki, Cushman, 1920, U.S. Geol. Survey, Prof. Paper, No. 125-D., pp.41. 42. pi. 7

Flat forms with umbo. Surface papillate. Radial length of the equatorial
chambers at 2 mm from the center 74 /x to 130 The largest chambers at
the periphery measuring 185 Embryonal apparatus of the quot;nephrolepidinequot;
type, measuring 0.110 mm x 0.150 mm to 0.330 mm x 0.37 mm. Diameter
4.1 mm to 10.2 mm, thickness 0.90 mm to 1.80 mm.

Lenticular form of the test. Surface weathered. Radial length of the
equatorial chambers at 2 mm from the centre 40 /x to 55 /z; at the periphery
75 /X. Diameter 5.1 mm, thickness 1.8 mm. Embryonal apparatus consists
of one big chamber encirchng a smaller one. Diameter of the bigger chamber
0.26 mm.

Upper Eocene, Pinar del Rio, Cuba. Hypotype, Min. Geol. Inst
Univ. Utrecht. D. 14774.

Clypeaster lanceolatus, Cotteau, Cotteau Bol. Com. Mapa Geol. Espafta vol. 22, p. 39, plate 9, figs.

This specimen was found at V. 774 N.E. of San Cristobal. The test
measures 75 mm length, 63 mm in width, about 20 mm in height and is
rather well preserved. The apical disk is slightly broken although two
genital pores are distinctly visible. Poriferous areas are narrow, slightly
depressed, terminating in a closed point, each of the plates bearing 4 to 5
tubercles. The 5 ambulacral furrows are not visible because they are too
much covered with limestone.

CoTTEAU describes his type as Miocene, Matanzas, Cuba; so does
Lambert with his species from Antigua. According to Jackson, who
studied specimens from Panama U.S.A. and Havana, Cuba, they should be
aged as Oligocene.

Antillasur arnoldi, Clakk, Memoirs of the Museum of Comp. Zoology at Harvard CoUege Vol. L. No. 1,

This specimen measures 70 mm in height, the length and width are
rather doubtful as the specimen is squeezed together somewhat on one
side. Apical system defective because the specimen is broken all over the
test, but it corresponds fully with the description of H. L. Clark.

It was found sohtary at V. 699 N.E. of Consolacion Del Sur, in an
area where the Upper Cretaceous Havana formation is exposed. However,
it might be easily derived from the adjacent lower Tertiary strata.

In the Aptychi limestones of Northern Santa Clara, Rutten (64)
mentions the occurrence of oil seeps. The equivalent of these beds in Pinar
del Rio are the younger parts of the San Andres formation. In the limestones
of this formation we also found traces of oil, while a strong bituminous
odour is often stated at fresh breaks. On account of the strong orogenetic
activity, to which these oil bearing limestones were exposed, no accumu-
lation of oil is to be found in them. The existing overthrust planes do
not seem to fulfil the conditions for economic accumulation.

At several places, e.g. at Cacarajicara, South West of Bahia Honda
and at loc. V. 804 (Mina Mariel), North East of Cayajabos, asphalt is mined.
The asphalt is found concentrated along faults in the Habana formation
and the Lower Tertiary strata. In all probability, the asphalt has been
derived from the oil-bearing limestones of the San Andres formation.

Ore deposits are found numerously in the province of Pinar del Rio
An important Coppermine is found at Matahambre. We cannot suggest
a theory on the origin of this ore. The chalcopyritic ore is worked to a
depth of 700 m. Rocks adjacent to the ore bodies, proved to consist of a
quartzitic rock not to be distinguished from the quartzites of the San Andres
formation, in which the mine is situated. The levels in which the rounded
ore bodies occur cut the strata obliquely. The main level is directed
N 42° E., dipping 45 degrees to the West, while a large, transverse fault
is found. The management of the Matahambre mine gave a member of our
expedition a private report for perusal in which L. C. Graton, of Harvard,
makes use of the existence of Cubanite and possibly Pyrrhotite to prove
the hypothermal origin of the copper ores.

In the older literature we found some communications about the
Matahambre mine and some information on nowadays unimportant ore
deposits. They will be mentioned in the chapter on Previous Literature.

Various courses through the Eastern part of the province of Pinar del
Rio will be described in detail in this chapter. No courses through the
Western part are described as the rather monotonous San Andres formation
does not give geological details, which have not already been discussed in
chapter II The different findspots of Upper Cretaceous Habana formation
in these Western parts have also been for a part mentioned already.

About one km West of Caimito on the Carretera Central we turn to
the North. We pass through an area consisting of white to grey porous
limestones At loc. L. 999 the limestones contain Lithothammum, Globi-
gerines and other small, indeterminable Foraminifera. North of this spot
we find limestones and marls of Eocene age ; the former contain Lepidocj-
clina and Discocyclina. Near loc. L. 1002 we find badly exposed Serpentines,
followed by a dark grey breccious limestone of Maestrichtian age ; a thin-
section of this breccia carries Rudists fragments and an uncertain
Vauzhanina (Loc. L. 1003). The road runs through a second area of Serpen-
tine and through outcrops of dark blueish limestones resembhng the lime-
stones of the San Andres formation. Paléontologie evidence estabhshing

Turning to the South we again reach the region of white hmestones
marls and calcareous sandstones of Upper Cretaceous or Lower Tertiary
age A loose big fragment of a Rudist {Parastroma) has been coUected at
loc. L. 1004. The right side of the road is covered with large boulders
of quot;blue limestones, indicating a nearby boundary of the_ San Andres
formation. To the West we pass into this formation, consisting here of
strongly folded shales with intercalated grey-blueish limestones. Fram
loc. L. 1005 to loc. L. 939 we find the Upper Cretaceous-Lower Tertiary
sediments well exposed. The direction of the strikes in these sediments
varies strongly. The dips run from horizontal in Oligocene limestones at
loc. L. 941, carrying eulepidine Lepidocychnes, to 80 degrees in other

On the Carretera Central halfway between Caimito and Guanajay
(loc. H. 971) Foraminifera of Oligocene age were collected {Lepidocjclina
favosa, Lepidocjclina dilatata, Lepidocjclina piedrasensis and Camerina petri).

A survey of the Loma Anafe North of this locality did not yield any
Foraminifera establishing its age. The hills consist chiefly of white lime-
stones, developed as quot;Dientes de perroquot;. At loc. A. 712 a thin-section of

a white hmestone contains Amphisorus matleyi, indicating the young Oligo-
miocene covering. South of this locality, however, we find dips of 20°—30°
in the limestones, which implies a Lower Tertiary age.

North of the Carretera Guana] ay-Cabanas on the road from Martin
Mesa to Mariel we find a large outcrop of Serpentine (harzburgite). At
loc. L. 983 we pass into the blueish limestone and red shales, which are
reckoned to the San Andres formation by us on account of the great
resemblance with rocks of this formation. Paleontologic evidence is lacking.
The limestones mainly dip 50°—60° to the South. Folded or wedged in the
limestones we find calcareous sandstones of Maestrichtian age containing
porphyrite material and Rudists fragments. About 150 m North of this
outcrop an anticjine occurs in the limestones of the San Andres formation;
the northern part of this anticline is covered by a gray-blueish Hmestone-
breccia of Upper Cretaceous age (loc. L. 985 carries Rudists fragments,
Orbitoides and Vaughanina). The same limestone-breccia was noted in the
field in two other places North of loc. L. 985 wedged into beds of greenish-
blue limestones, gray limestones, blueish limestones cut by calcite veinlets
and shales of the San Andres formation. An outcrop of Serpentine is found
at loc. L.988. 400 m North of loc. L.989, at the Northern boundary of
the San Andres formation, a siliceous sandy shale is found ; we then pass
into an area covered with gray earth and without any exposures as far as
loc. L. 990, where we come into the Oligomiocene cavernous limestones,
which continue till we reach Mariel.

The village of Bahia Honda is situated in the Tuff Series. On the spot,
where the road to El Rosario turns off from the main street, we find an
outcrop of strongly weathered diabase. To the South at loc. M. 1034 small
dikes of gabbroid nature occur. A patch of Serpentine is found at loc.
M. 1037. We then pass through a steep syncline of fine conglomeratic
calcareous gray-white sandstones (Habana beds in Eastern facies) carrying
at loc. M. 1038 Vaughanina, Orbitoides, small Camerinas and dioritic
material. It is bordered by a Serpentine area and gabbroid rocks, which
may be continued in Eastern and Western direction, forming a large sill,
parallel to the general strike in the Tuff Series. The latter consists of partly
siliceous, vitric tuffs, thin bedded cherts, porphyrites, shales and grayish-
blue limestones. These strata show a constant dip to the North from 40°
to vertical. In two localities, M. 1046 and M. 1049, we find outcrops of
breccious limestones and conglomeratic calcareous sandstones of a dark
gray-blue colour (Habana beds of Mountain facies). The rocks carry rounded
fragments of porphyrite and porphyrite matrix, dioritic material, rounded

fragments of phyllites and quarzites ; the chief component being fragments
of dark gray-blue limestones. Both localities carry Rudists fragments,
Orbitoids and probably Vaughanina, indicating an Upper Cretaceous age.
These strata, in which strike and dip are not to be measured we take to
have been wedged into the older Tuff Senes during the post-Maestrichtian

anymore. We then pass into the younger parts of the San Andres formation,
coListing of thinly bedded and compact blueish-gray hmestones shales
and cherts, sandstones and quartzitic sandstones; all beds constantly dipping
to the North. These decidedly intercalated sandstones or quartzites show
a great resemblance with the rocks found West of San Diego de los Banos
in the probably older parts of the San Andres formation. At loc. V 868,
a small layer'of sandstone is intercalated in blueish-gray hmestones
carrying Ammonites and Aptjchi of Lower Cretaceous age. At loc V. 858
and V. 873 small sttips of Serpentine are exposed. Three outcrops of Upper
Cretaceous rocks are found in these parts of the San Andres formation.
The findspot \ km South of loc. M. 1050 consists of dark blue biturmnous
limestone-breccia carrying Rudists fragments, Orbitoids and porphyntic
matrix. The existence of HgS gas in this locality points to a tauit or a
overthrust. At loc. V. 863 we find a coarse conglomerate, contammg rounded
pebbles of tuffaceous, ? diabasic origine. South of the Serpentine outcrop
at loc V. 873, we find again the bituminous limestone-breccia (loc. V. 875)
carrying Rudists fragments and Orbitoids, limestone fragments contaimng
Miliolids and clear quartz. The outcrops of Habana beds m Mountam facies
in the San Andres formation are infoldings or more probably wedges.
The Serpentines often found near the Habana beds acted as a shde-
expedientquot;, the contacts in that case being tectonical ones.

We pass through the Oligomiocene area. Several outcrops of white,
cavernous limestones carry the typical fauna for these beds (Iocs M. 1007
H. 895: Miogypsina, Archaias, Amphisorus matleyi). At oc. H. 896 we find
white compact limestones of Upper Eocene age in which are found in thin-
sections Asterocyclina, Discocyclina, Miliolids, and Operculina.

At the foot of the Sierra de los Organos we find loose boulders of a
grayish limestone-breccia; they contain Rudists fragments recrystallized
Orbitoids, fragments of gray-blueish limestones, rounded fragments of a
suboolitic limestone and a phyllite fragment. Assuming that these boulders
are not transported, we have at this spot (loc. M. 1009) the same Mountam
facies of the Habana beds which is found at the overthrusts m the older
formations. They are deposits in shallow water, their mam elements (blueish
limestones) are derived from the adjacent surroundings only partly emerged.

of strongly folded grayish blue calcareous shales and limestones, dipping
40° to the North to vertical.nbsp;^

A very coarse diabase rock containing enclosures of marble is found
at loc. M.1013. We take this rock to be connected with the Tuff Series
breakmg through the older San Andres formation.

Aptychi, indicating a Lower Cretaceous age for these parts of the San
Andres formation, were found about 2 km West of loc. M. 1013.

Near loc. A. 760 limestones and cherts of the San Andres formation
alternate with beds of the Habana formation, consisting here of a blue
limestone-breccia carrying Orbitoides hrowni. At loc. A. 763 we find
limestones alternating with sandstones (Cayetano facies); the strata
generally dip to the North.

North of loc. A. 766 occurs an outcrop of Serpentine rock over a
distance of about 600 metres. In this Serpentine area were sampled rocks
of a spilitic-diabase nature, which are difficult to account for. The pendotitic
magma probably followed the same course as a former magma, connected
with the Tuff Series, of which rcHcs are found now as inclusions in the
Serpentine. At loc. A. 770 a gabbro-diabase and an amphibolitic rock were
collected in the limestone area, which is strongly folded and dipping to the
North and to the South.

A limestone breccia of uncertain Upper Cretaceous age occurs at loc.
A. 771 I. It contains e.g. fragments of a suboolitic limestone. North of this
outcrop serpentinized rock breaks through sandstones of Cayetano facies,
carrying inclusions of porphyritic rock, chloritic rock and amphibolites
of large dimensions (the largest being about 1 cbm). The chloritic rock and
the amphibolites are not considered to be altered rocks of the Tuff Series,
as no sign of metamorphism is found at the contacts of the peridotitic
magma with the Tuff Series. We prefer indicating these rocks as of
quot;unknown originquot;.

North of the Serpentine we find again the Habana beds, the limestone
breccia carries Rudists fragments, Orbitoids and Torreina indicating a
Maestrichtian age. At loc. A. 775 occur calcareous shales and a chert-
breccia, which is reckoned to the San Andres formation.

From Artemisa the road runs through a level country. Outcrops are
sparse, and the ground is covered with a red soil. Past loc. L. 923 the
quot;Guinnessquot;-Hmestones of Oligomiocene age are exposed. South of the
town Cayajabos (loc. L. 931) occurs an outcrop of yellow crystalline
limestones, carrying recrystallized Orbitoids, too badly preserved for
determination.

In the main street of the town strongly folded cherts arc well exposed,
the beds dip to the South and to the North. 400 m North of the last outcrop
of chert we find an exposure of a coarse weathered diabase. We reckon the

diabase and the cherts to the Tuff Series. The connection of this Tuff Series
area with the Tuff Series beds situated in North-Western direction, is not

The road then runs through a large area of limestone-breccia, conglo-
merates white and yehow marls and calcareous sandstones. No fossils,
indicating the age of these strata were found, but we may safely assume
them, on account of the general appearance, to be of Upper Cretaceous or

and vitric tuffs, followed by steeply folded beds of Upper Cretaceous or
Eo-Oligocene age. Tuffaceous beds South of San Juan Batista are badly
exposed on the road. About one km to the West, we have clear evidence
of them. At loc. H. 880a conglomeratic sandstones occur, carrying badly
preserved Orbitoids and Miholids, and fragments of dioritic and porphyritic
material. They are part of the Upper Cretaceous to Lower Tertiary strata,
consisting further of white chalks and calcareous brown sandstones. The
beds are gently folded ; the strike running in East-West direction. They
continue tih we reach Cabanas.

We leave the town of Bahia Honda in a Western direction. Along the
road we find outcrops of strongly weathered tuffaceous rocks. South-West
of the town the hills consist of white marls of the Upper Cretaceous or

We run into the Tuff Series, to which is reckoned a chert area extending
from loc. H.951 to loc. H. 948, dipping generally to the North with
occasional intercalations of limestones lenses. Rocks of tuffaceous nature,
diabases, porphyrites and glass porphyrites have been collected at various
places. (Iocs. H. 933, H. 934, H. 935, H. 936, H. 943). Also shales are
often exposed in this area. An old abandoned copper-mine (Mendietta)

In the neighbourhood of Cacarajicara numerous outcrops of blueish
conglomeratic limestones and calcarous sandstones of Upper Cretaceous
age occur (Iocs. H. 904, H. 906, H. 923, H. 932). Strikes and dips are not
measurable as is always the case in the Habana beds of Mountain facies.
A fault in which asphalt is found runs in a North-South direction. Two
Orbitoids bearing limestone-breccias are found to the South, respectively
at loc. A. 684 and at loc. A. 685.nbsp;^ t y

All the Upper Cretaceous limestone-breccia strata are taken to be
wedged into the San Andres formation.

South of loc. A. 685 red and yellow sands indicate a frequent inter-
calation of sandstones (Cayetano facies) in the San Andres formation.
North of Sabanilla we find large boulders of Serpentine (loc. A. 686).

The strata South of Sabanilla, consisting chiefly of limestones, continue
to dip to the North til we reach loc. A. 658, South of which the beds dip
to the South. At loc. A. 658 a quartzite is found, intercalated in the lime-
stones. This rock is not to be distinguished from the quartzites found
West of San Diego de los Banos.

at loc. A. 656 and loc. A. 654. We take these beds to be of Upper Cretaceous
age by their general appearance.

Aptychi occur at loc. A. 653, establishing a Lower Cretaceous age for
these parts of the San Andres formation (Trauth, 79).

A dubious Serpentine outcrop is found at lo'c. A. 651 ; then we leave
the mountain region. The red soil is covered by gray limestone-boulders
and chert fragments derived from the San Andres formation. Near loc
L.842 a conglomerate contains porphyrite boulders; it is reckoned to the
Upper Cretaceous or Lower Tertiary.

At loc. L. 841 and L. 839 Oligomiocene limestones are exposed. They
carry its typical fauna: Amphisorus matleyi, Archaias, Miogypsina and
Miliolids.

There are numerous publications in existence, treating the geological
problems, ore deposits or paleontological matters, concermng the provmce
ITv lZ del Rio A great part of these papers were not accessible to us, as
therare not found In any library ia Holland However, P-f. Rutten
gave us for perusal his bibliographic notes on the geology of Cuba, which
LIbled us to give short summaries of those parts of the pubhcations,

In 1884 Castro (14) mentions the occurrence of dark Jurassic lime-
stones outcropping from Guane to SoutbWest of Guanajay He advances
^e opinion, th^at Hmestone conglomerates, found ^e^ -f^^e t^
Pinar del R o and in a small zone South of San Diego de los Banos, might
bfof Cretaceous age, on account of the possible occurrence of Rudists. In
the same year a gedogieal map was pubhshed by Castro and Salterain y
LegarT On this map we find Paleozoic, Mesozoic and Tertiary formations
indkatedVn the province of Pinar del Rio. Apart from the quot;Quaternarioquot;
also igneous rocks are indicated (Granito, Serpentina, Basalto).

Also in 1884 Salterain y Legara (65) records an earthquake on the
22nd and 23rd of January 1880 in the towns of San Cristobal and Cande-

^^quot;'in 1909 de la Torre (76) states the occurrence of Ammonites near
Vinales, while in 1909 (77) and 1910 (78) the Jurassic age of the fauna is

1908'L'iquot;ETT (15) describes „Cambricquot; shales and slates situated
25 miles West of the town of Pinar del Rio. The formation is folded and
injected by quartz veins. On the axis of the anticlines iron ore is found.
The ore is hematite, in which baryte crystals occur.

In 1916 Ortega (55) mentions the occurrence of Jurassic-Cretaceous
limestones, with intrusive and covering basic eruptive rock, covered once
more by limestones, shales and sandstones. The copper ore of the Mata-
hambre mine is said to be connected with the Serpentine. The ore would
have been formed by desagration of the Serpentine rock, by the circulation

Corrections of the map of de Castro and Salterain y Legara appear
in 1917 (Anonymus 4). A large Serpentine area is wrongly sketched-in
North of Vinales. A large strip of Serpentine rock is sketched-in running
from San Diego de los Banos to North of the town of Pinar del Rio.

Another publication in 1917 (Anonyaius 5) deals with the results ot
drilhng for oil. At Morillo, South East of Bahia Honda a well was sunk to

a depth of 1841 , praetieaUy passing only through Serpentine roek. Traces
of oil and gas were found. The San Felipe well, 1.5 miles South West of La
Esperanza also runs through the Serpentine to a depth of 1391'. No gas
or oi was found At about a distance of one mile from the Mina Markl,
a well was dril ed to 1850' Only a little liquid asphalt was found. At La
Esperanza a well was drilled entirely through limestones (Medina Oil Cy.).
Gaston (33) reports also in 1917 the occurrence of gas and asphalt in a
well m the mine quot;Santa Mariaquot; on the North coast of Pinar del Rio, near
luerto Esperanza. The depth of the well was about 1600'

Hayes c s. (38) republish the map of Castro and Salterain y Legara,
together with a po ogical survey of Cuba. A large part of the Organos
mountams is still taken to be Paleozoic. The Jurassic limestones of Vinales
are known to them. In the North of the province of Pinar del Rio, Eocene
mght occur. Upper Oligocene is reported 6 km North of the town of
iinar del Rio and at Consolacion del Sur. The paleontological evidence
on which these statements are based are not mentioned. Miocene or Pliocene
are in all probability absent according to them.

Mac Cormick (47, 48) and Corral (19) give in 1918 some, partly
technical details on the Matahambre mine. When treating the mine quot;La
Nina and quot;Mina Concepcionquot;, Corral (20) describes Serpentine between
La Palma and Las Pozas. The Serpentine is considered to be the marginal
facies of a hypothedcal granite. In two publicadons Brown and O'ConSell
treat the Ammonites and the strata from which they are collected (11 12)
In the last publication sections through the Organos mountains are given.'
These sections run to the North from the towns of: Candelana? San
Cristobal, San Diego de los Banos, and Vinales. A section from Candelatia
or San Cristobal to the North is said to pass through recent or pleistocene
deposes in the plain, then through Miocene and Oligocene beds followed
by thick Cretaceous limestones and Jurassic beds, the latter forming the
Mountain regions (full discussion in our text).

In 1919/20 Burchard (13) mentions the occurrence of manganese
ore near Vinales and Mendoza.

In 1920 Brown (10) wrote a private report which has been cited in
the literature from time to time. According to a statement of Mr. Brown
this report has never been published.

Suarez-Murias (72) reports in 1920 the occurrence of Jurassic for-
mations and younger basic eruptive rock in Pinar del Rio. The basic rock
consists of Serpentine, dionte and andesite. These rocks contain sediments
as xenoliths. He mentions unimportant magmatic copper-ores and lateritic
ore in the Serpentine districts.

In 1923 Allende (2) desctibes 6 zones running parallel to the anticlinal
axis of the mountains, in which minerals are found. Peridotites carrying
sulfides of Fe and Cu are reported from Sabalo, in the valley of San Juan y
Martinez, Valle y Realengo de Lagunillas, Rio Hondo etc. A formation
quot;plumbo-bariticaquot; is found between Bolondron and Isabel Marie. Iron-

^ In 1928 the same author (2a) mentions the localities where traces of
oil or asphalt have been found in the province of Pinar del Rio. This is the
case at: Arroyo de Mantua and between this place and Dimas and near
Puerto Esperanza at Las Playelas. An asphalt mine lt;'E1 Murilloquot; occurs
in the neighbourhood of La Mulata; Asphalt at Cacarajaicara; Traces of
oil near Asiento de Echevarria (Cretaceous shales), at the Loma de Rangel
and in the hills of San Cristobal and Candelaria, and along the nver San
Cristobal. Oil is found on the finca Cbvadonga near San Juan y Martinez,

^^^ ciADO^in 1923 (16) gives information on the mines quot;Las Mercedasquot;
and quot;Maria Christinaquot; both near Guane. In the former, copper ore was

Wright and Sweet (85) discuss in 1924 the asphalt mine quot;Manel .
The asphalt must have been reduced from 20-30 mil ion barrels of primary
oil The oil is considered to have been derived from the Jurassic limestones.

■ In 1932 Whitney Lewis (44) discusses the geology of Cuba and pu-
blishes a geological map. By comparison the reader will see e^ential diffe-
rences with om map. They are too numerous to discuss here. Regarding
the Vinales limestones Lewis considers them to rest unconformably upon
the quot;Pinar schistsquot;. Cretaceous beds are reported to occur near Mariel,
Cabanas and Bahia Honda. Another publication of the same author m the
same year, (46) treats the age of the Aptydi occurring in the hmestones.

In 1934 Weisbord (84) describes Echinoids collected on the road
between SanDiego de los Bahos and Paso Real. He mentions the occurrence
of Upper Eocene in the heart of the Organos mountains (personal com-
munication of Mr. W. H. Butt).

In 1935, Schuchert (70) publishes a large study on the ' Historical
Geology of the Antillean-Caribbean regionquot;. Cuba is extensively treated

Dickerson and Butt (30) in the same year treat the problems of the
quot;Cuban Jurassicquot;, which paper has been fully discussed in our text.

The publications of L. Rutten (60, 61, 62), of M Rutten (63, 64)
and of Thiadens (73, 74) are based upon evidence collected during our

Bol. Com. Mapa Geol. Espana, XX, (1893) 1895, pp.
71—88. Lam. I—IV.nbsp;' ^ ^ 'FF

Rio, basado en el croquis geológico de la Isla de Cuba por
Manuel Fernandez de Castro y Pedro Salterain y Legara
con las adiciones y modificationes introducidas por la
Jefatura del Distrito de Pinar del Rio. Bol. de Minas.
Habana 2.

que la Isla de Cuba ha estado unido al continente Americano
y breve idea«de su constitución geológica. An. Ac. Habana
21, pp. 146—165.

ri6^ Cayado Enrique, 1923: Informe del Negociado de Mmas referente
(16) cayado, li ^^nbsp;realizados y al movimiento de asuntos

mineros habido en la Republica desde el 1° de Enero hasta
el 31 Diciembre del ano 1922. BoL de Mmas, Habana, 7,

(23)nbsp;Cushman, J. A., 1919 : Fossil Foraminifera f^om f ^ ^est Indies,
^ Carnegie Inst., Publ. 291, pp. 23-7 , 5 pis.

(30)nbsp;Dickerson, Roy, E. and Butt, W. H., 1935 : Cuban Jurassic. Amer.
^ ^ Assoc. Petrol. Geol., Bull. vol. 19, no. 1, pp. 16-118.
(3\) Ellis BE 1932 : Galloivafina bromu, a new genus and species ot

' orbitoid from Cuba, with notes on the American occurrence
of Omphalocjclus macropora. Amer. Mus. Novitates, no. 568,
8 pp., 9 figs.

Pinar del Rio durante el segundo semestre de 1916. Bol.
de Minas, Habana, 3, pp. 4—14

description of a new species from Cuba. Tour. Amer. Pal
IV, pp. 268—270. pl. 22.

from the Moody's Branch mad, Jackson Eocene, of Texas,
Louisiana, and Mississipi. Jour. Paleontology Vol 9
no. 4. pp. 327—340, pis. 29—32.

with an arrangement of the Families of Holostean Ganoid
Fishes. Bull. Amer. Mus. Nat. Hist., 48, 8, pp. 223—242

sobre un reconocimiento geológico de Cuba. Bol. de
Minas, Habana, II, pp. 1—63, III, pp. 63—132.

physiography and general geology from the quot;Report on a
geological reconnaissance of Cuba 1901quot;, Habana.

Soc. Acad. d'Agriculture, des Sciences et Belles Lettres du
Departement de l'Aube, Troyes, vol. 79, pp. 17—34.

râneas de la meséta central de Cuba. An. Acad. Ciencias,
Habana, 63, pp. 41—71.

(50) O'Connell, marjorie, 1919: Orthogenetic development of the
^ ^nbsp;Costae of the Perisphinctinae. Amer. Jour. Science, (4),

XLVIII, pp. 450—460.
/^jN__ 1920 • Further studies on the Jurassic of Cuba. Geol. Soc.

C55^ Ortega P 1916 : Ojada retrospectiva y resena sobre el estado
' actual de la minen'a en Cuba. Bol. de Minas, Habana, I,

(56) Palmer, Dorothy, K., 1934 : Upper Cretaceous age of the Orbitoidal
^ ^nbsp;genus Gallowayina Ellis. Geol. Soc. Amer., Proc. 1933.

' Gallowafma. Ellis. Jour. Paleontology, 8, pp. 68—70.
(59) Palmer, R. H., 1934 : The geology of Habana, Cuba, and vicmity.

Jour. Geol, vol. 42, pp. 123-145.
r60) Rutten, L., 1934: Geology of Isla de Pinos, Cuba. Kon. Akad.
^ ^nbsp;Wet. Amsterdam, Proc. Vol. XXXVII, no. 7, pp.

'de la comisión cientifica holandesa en Cuba. Rev. Soc.
Geogr. Cuba, Afio VI, Num. 3, pp. 47—52.
(63) Rutten M. G., 1935 : Larger Foraminifera of Northern Santa Clara
Province, Cuba. Jour. Paleontology, Vol. 9, no. 6, pp.
527—547, pis. 59—62.

Geol. Reeks, no. 11.
(65) Salterain, Pedro y Legara, 1884 : Ligera resena de los temblores
de tierra occurridos .en la Isla de Cuba. An. Acad. Habana,
XXI, pp. 203—218.

' de inspección a las minas de las provincias de Pinar del Rio
y Habana. Bol. de Minas, Habana, IV, pp. 69—76.

(69)nbsp;Schlumberger, Ch., 1901 : Preniière note sur les Orbitoides, Soc. Géol.

comprendida entre Bahia Honda y la Palma, provincia
Pinar del Rio. Bol. de Minas, Habana, 6, pp. 29—32.

dans la région occidentale de Cuba. C. R. Congr. Int. Geol.
XI, pp. 1021—1022.

Foraminifera from Jamaica. Jour. Paleontology, vol. 3,
no. 4, pp. 380—382, pi. 41-^9.

scource of oil in Western Cuba. Amer. Assoc. Petrol.
Geol., vol. 8, pp. 516—519.

2, Vertical section showing the embryonal apparatus,
X 15. 3, Tangential section showing the pores in the
apertural band, X 19.

De meening van Holwerda, dat in den Romeinschen tijd
een eilandènre^s in de „Hoofdenquot; gelegen zou hebben, moet

t van Veen- Onderzoekingen in de „Hoofdenquot; iii verband
j. vannbsp;•nbsp;i 1 der Nederlandsche kust. Nieuwe ver-

halel njen an Lr Bataafsch Genootschap der Proef-
Il'dtvindelijke Wijsbegeerte te Rotterdam. 1936.

Ten onrechte wordt Tampsia lopcztrigoi door Palmer tot
het genus Tampsia gerekend.

De ontstaanswijze van het Bovcn-Engadiner dal door fluvia-
tiele ero^is aannemelijker dan door tectomsche oorzaken.

De kwartsitische gesteenten, welke in de syenitische
hoornblenditische (appinidsche) eruptiva te Colonsay voor-
komen, moeten als xenoHethen opgevat worden.

Men mag het ontstaan van den yogelttek niet in verband
brengen mft invloeden van de D.luv.ale .)SÜ,den.

f Mayfr en W. Meise: Theoretisches zur Geschichte des
^ V^ilzuges Der Vogelzug, No. 4, I- Jahrgang, 1930.

De aan.ve.igheid - r'^^MofS.quot;^^^^^^^^^
^eToÄ^r^^^ Ïge?r Boven-Senonen ouderdom
van deze lagen.

De schisten op Jamaica worden ten onrechte door Matley
voor Paleaozoisch gehouden.