GeolCarp_Vol64_No3_195

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, JUNE 2013, 64, 3, 195—208 doi: 10.2478/geoca-2013-0014

Introduction

The location of Cuba within the Caribbean plate, offers a good
point of reference to compare and establish links between the
geological and biological processes in the Eastern and West-

Calpionellid distribution and microfacies across the Jurassic/

Cretaceous boundary in western Cuba (Sierra de los Órganos)

RAFAEL LÓPEZ-MARTÍNEZ

, RICARDO BARRAGÁN

, DANIELA REHÁKOVÁ

and

JORGE LUIS COBIELLA-REGUERA

Instituto de Geología, Universidad Nacional Autónoma de México, Ciudad Universitaria, Delegación Coyoacán, C.P. 04510, México

D.F., México; rafaelopez83@hotmail.com

Comenius University, Faculty of Natural Sciences, Department of Geology and Paleontology, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; rehakova@fns.uniba.sk

Departamento de Geología, Universidad de Pinar del Río, Martí # 270, Pinar del Río, C.P. 20100, Cuba

(Manuscript received May 21, 2012; accepted in revised form December 11, 2012)

Abstract: A detailed bed-by-bed sampled stratigraphic section of the Guasasa Formation in the Rancho San Vicente
area of the “Sierra de los Órganos”, western Cuba, provides well-supported evidence about facies and calpionellid
distribution across the Jurassic/Cretaceous boundary. These new data allowed the definition of an updated and sound
calpionellid biozonation scheme for the section. In this scheme, the drowning event of a carbonate platform displayed
by the facies of the San Vicente Member, the lowermost unit of the section, is dated as Late Tithonian, Boneti Subzone.
The Jurassic/Cretaceous boundary was recognized within the facies of the overlying El Americano Member on the basis
of the acme of Calpionella alpina Lorenz. The boundary is placed nearly six meters above the contact between the San
Vicente and the El Americano Members, in a facies linked to a sea-level drop. The recorded calpionellid bioevents
should allow correlations of the Cuban biozonation scheme herein proposed, with other previously published schemes
from distant areas of the Tethyan Domain.

Key words: Jurassic/Cretaceous boundary, Cuba, calpionellid biostratigraphy, microfacies, drowned platform, storm
deposits.

tributed  to  the  topic,  especially  Furrazola-Bermúdez  &
Kreisel (1973), who recognized the presence and stratigraphic
distribution  of  the  Crassicollaria  and  Calpionella  Zones  in
some sections of western Cuba, and reported a new species
of  Chitinoidella.  However,  in  their  study,  they  did  not  pro-

Fig. 1. Map showing the location of the Rancho San Vicente stratigraphic section and the main tec-
tonic units and structures of western Cuba. Modified from Cobiella-Reguera & Olóriz (2009).

ern Tethys during the Mesozoic,
particularly those at the Juras-
sic—Cretaceous  interval.  Sev-
eral  good  successions  of  the
Tithonian/Berriasian  boundary
interval  of  western  Cuba  are
well-exposed  in  the  Pinar  del
Río  Province.  They  are  essen-
tially  recorded  on  the  Guasasa
Formation,  a  typical  unit  of  the
San  Vicente  stratigraphic  sec-
tion  at  “Sierra  de  los  Órganos”
orogenic belt (Fig. 1).

Pioneering works on the def-

inition  of  the  Jurassic/Creta-
ceous  boundary  in  western
Cuba  on  the  basis  of  ammo-
nites,  calpionellids  and  other
microfossils  were  focused  on
stratigraphic sections across the
“Sierra  de  los  Órganos”.  The
first

contribution

was

Brönnimann in 1954. Since
then, several authors have con-

196

LÓPEZ-MARTÍNEZ, BARRAGÁN, REHÁKOVÁ and COBIELLA-REGUERA

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

duce sound data to establish the Jurassic/Cretaceous bound-
ary  in  Cuba  by  means  of  calpionellids.  Later,  Pop  (1976)
analysed  three  sections  in  the  “Sierra  de  los  Órganos”  belt
defining calpionellid zones and concluded that the Jurassic/
Cretaceous boundary in this area could be established at the
base  of  the  Calpionella  Zone.  Pszczółkowski  (1978)  subdi-
vided the Guasasa Formation into four members, namely in
stratigraphic order: San Vicente, El Americano, Tumbadero
and  Tumbitas.  That  author  placed  the  contact  between  the
San  Vicente  and  El  Americano  Members  as  coincident  with
the  Kimmeridgian/Tithonian  boundary,  whereas  the  contact
between the El Americano and Tumbadero Members was con-
ceived as coincident with the Tithonian/Berriasian boundary.
Myczyński  &  Pszczółkowski  (1990)  kept  the  El  Americano/
Tumbadero contact as coincident to the Tithonian/Berriasian
boundary on the basis of ammonites and microfossils. How-
ever, Fernández-Carmona (1998) in his unpublished Doctoral
Thesis  placed  the  Tithonian/Berriasian  boundary  within  the
uppermost  strata  of  the  El  Americano  Member.  Afterwards,
Pszczółkowski  &  Myczyński  (2003)  pursued  and  accepted
that idea for some sections in western Cuba.

Pszczółkowski et al. (2005) identified calpionellid and

radiolarian  zones  in  western  Cuba  and  correlated  them  with
ammonite  zones  from  the  western  Tethys.  The  last  relevant
contribution to this topic in western Cuba is by Pszczółkowski
&  Myczyński  (2010),  who  analysed  calpionellid  and  ammo-
nite assemblages, but no differences in age of the members of
the  Guasasa  Formation,  neither  the  stratigraphic  position  of
the Jurassic/Cretaceous boundary within the unit were reported.

The present contribution focuses on calpionellid bio-

stratigraphy from the San Vicente to Tumbadero Members
within the Guasasa Formation in the San Vicente Section of
the “Sierra de los Órganos”. In order to specify the age of the
limits between its members, and to establish a reliable posi-
tion of the Tithonian/Berriasian boundary within the unit,
this work was based on a high resolution sampling.

Regional geological setting

According to Iturralde-Vinent (1997), the stratigraphy of

Cuba can be differentiated into two main domains associated
with different geological histories: the foldbelt (Early—Middle
Jurassic  to  Late  Eocene)  and  the  neoautochthonous.  The
foldbelt is composed of elements detached from several old
tectonic  plates,  while  the  neoautochthonous  was  formed  in
the  North  America  Passive  Margin  after  the  accretionary
process that led to the formation of the foldbelt.

The nappe pile of the Guaniguanico Cordillera (Hatten

1967;  Khudoley  &  Meyerhoff  1971;  Piotrowska  1978;
Pszczółkowski  1978,  1994)  is  a  great  lens-shaped  antiform
with five main tectonic sheets, each one with its own strati-
graphic sections (Cobiella-Reguera 2008). Pszczółkowski &
Myczyński (2010) referred to this nappe pile as the “Guani-
guanico megaunit” in which the Sierra de los Órganos occu-
pies  the  lowest  structural  position,  whereas  the  Sierra  del
Rosario unit contains the uppermost nappes (Fig. 1).

In previous works the Mesozoic paleomargin sections in

the Guaniguanico Cordillera were considered as exotic crustal

blocks  or  terranes  (Iturralde-Vinent  1997;  Pszczółkowski
1999) detached from the Maya Block. In the opinion of other
authors, a good correlation between the Mesozoic sections in
the  southeastern  Gulf  of  Mexico  and  western  Cuba  sheds
new  light  on  the  idea  of  an  original  juxtaposition  between
both  domains  (Moretti  et  al.  2003;  Cobiella-Reguera  &
Olóriz 2009). However, Saura et al. (2008) considered west-
ern Cuban facies as a distal expression of the development of
the Bahamas-Florida margin.

Lithostratigraphy

The rock sequences of the Jurassic-Cretaceous boundary

transition in western Cuba are exposed in the “Sierra de los
Órganos”,  and  recognized  within  the  facies  of  the  Guasasa
Formation (Pszczółkowski 1978, 1999). This unit defined by
Herrera  (1961)  was  subdivided  by  Pszczółkowski  (1978)
into four members, which are named in stratigraphic order as
San  Vicente,  El  Americano,  Tumbadero  and  Tumbitas
(Fig. 2). Pszczółkowski & Myczyński (2010), correlated the
members with ammonites and calpionellid biostratigraphy as
shown on Fig. 3. In the section we studied, the upper part of
the San Vicente, the whole El Americano and Tumbadero and
the lowermost part of the Tumbitas Members are recorded.

San Vicente Member

This unit is of Kimmeridgian—Early Tithonian age accord-

ing  to  Pszczółkowski  &  Myczyński  (2010),  and  is  mainly
composed  by  massive  thick-bedded  shallow-water  carbon-
ates. A diagnostic feature of this unit is represented by par-
tially dolomitized limestones at the top. The fossils recorded
within this unit, mainly consist of Nerinea sp., Textulariidae
(Pszczółkowski  1978),  miliolids,  and  scarce  calcareous  di-
nocysts (Fernández-Carmona 1998).

El Americano Member

It is composed of thin-bedded limestones with shaly inter-

beds. The fossil record includes calpionellids and ammonites
in the topmost Tithonian and in the Berriasian (Fernández-
Carmona 1998; Pszczółkowski et al. 2005).

Tumbadero Member

It is represented by thin-bedded limestones of Middle—

Late Berriasian age with very thin cherty beds and lenses. A
rich association of radiolarians and calpionellids indicates
the pelagic origin of the limestones of this member
(Pszczółkowski & Myczyński 2003).

Tumbitas Member

It is mainly composed of thick-bedded, light microgranular

limestones, with a few clay interbeds. The field diagnostic cri-
teria to discriminate the Tumbadero and the Tumbitas Mem-
bers are the disappearance of the cherty lenses and the light
colour of the limestones. The stratigraphic section studied in
this work includes only a small lower part of this member.

197

CALPIONELLID DISTRIBUTION AND MICROFACIES ACROSS JURASSIC/CRETACEOUS BOUNDARY (W CUBA)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

Materials and methods

The present research focuses on the stratigraphic interval

from the topmost part of the San Vicente to the topmost part of
the Tumbadero Members. The sampling was done on a bed-
by-bed basis, including inter-layers. The samples RSV A—M
correspond to the San Vicente Member, RSV 1—95 to the
El Americano Member, and RSV 95—145 to the Tumbadero
Member (see Fig. 9 for detailed samples position).

Biostratigraphic results

Early Tithonian Semiradiata dinocyst Zone (Samples
RSV A—M)

These samples at the top of the San Vicente Member corre-

spond to the lower part of the studied section (Fig. 9). In thin
section the rocks are characterized as poorly sorted and washed
wackestones (occasionally non-fossiliferous mudstones) of in-
traclasts,  peloids  and  pellets,  alternating  with  peloidal  pack-
stones  (Fig. 4A).  The  main  skeletal  particles  are  benthic
foraminifers,  favreinids,  gastropods,  green  algae,  ostracods
and scarce bryozoans. Some samples are partially dolomitized
with euhedral dolomitic crystals; bioturbation is abundant prin-
cipally due to incrustation. The rock displays cloudy structure
in thin section due to microbial activity. Biostratigraphic indi-
cators  are  very  scarce  and  the  age  of  the  member  was  deter-
mined  only  by  the  presence  of  a  few  Cadosina  semiradiata
semiradiata Wanner (Fig. 4B) which could determine the Early
Tithonian Semiradiata dinocyst Zone sensu Reháková (2000a).

Late Tithonian

Chitinoidella Zone

Boneti Subzone (Samples RSV 1—5)

These rock samples from the very base of the El Americano

Member  (Fig. 9)  consist  of  saccocomid  mudstones  to  pack-
stones  with  less  abundant  filaments,  glauconitic  grains,  few
gastropods and echinoids (Fig. 4C—F). This interval is charac-
terized by the presence of Chitinoidella along with other gen-
era displaying microgranular calcitic walls looking dark under
a transmitted light microscope. The Chitinoidella Zone is di-
vided into two subzones namely from bottom to top as Dobeni
and  Boneti  Grandesso  (1977),  Borza  (1984).  In  the  analysed
section only chitinoidellids of Boneti Subzone were found.

Specimens of Chitinoidellidae are scarce, being represented

only  by  a  few  poorly  preserved  specimens  of  Chitinoidella
boneti Doben (Fig. 4G), Longicollaria sp. (Fig. 4H), Daciella
sp. (Fig. 4I) and Daciella danubica  Pop (Fig. 4J).  The  state
of  preservation  prevents  observation  of  diagnostic  features
of most of the specimens of this family. The matrix is always
microsparitic and masks other possible markers.

Nonetheless, this assemblage and the presence of Chiti-

noidella boneti  Doben, provide a good point to identify the
Boneti Subzone sensu Borza (1984). The absence of the un-
derlying  Dobeni  Subzone  is  explained  by  paleoecological
reasons  due  to  the  shallow-water  conditions  prevailing  be-
fore the drowning of the San Vicente carbonated bank.

Fig. 2. Correlation of Upper Jurassic and Berriasian lithostrati-
graphic units between the main tectonic domains of western Cuba.
Modified from Cobiella-Reguera & Olóriz (2009).

Fig. 3. Calpionellid and ammonite biostratigraphy of the Rancho San
Vicente section according to Pszczółkowski & Myczyński (2010).

199

CALPIONELLID DISTRIBUTION AND MICROFACIES ACROSS JURASSIC/CRETACEOUS BOUNDARY (W CUBA)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

The Boneti Subzone has been recorded with a similar as-

semblage from Cuba (Kreisel & Furrrazola-Bermúdez 1971;
Furrrazola-Bermúdez & Kreisel 1973), Mexico (Lugo 1975),
Western Balkanides (Bakalova 1977; Lakova 1993), Western
Carpathians (Borza 1984; Reháková & Michalík 1997),
Northwestern Anatolia (Altiner & Özkan 1991) and Eastern
Alps (Reháková 2002).

Late Tithonian

Crassicollaria Zone (Samples RSV 6—22)

An abrupt change in the facies occurs in this part of the

section  still  within  the  base  of  the  El  Americano  Member
(Fig. 9). The Saccocoma packstones are replaced by wacke-
stones  with  sponges,  radiolarians,  calpionellids,  filaments
and  scarce  resedimented  gastropods  and  bryozoans
(Fig. 5A,B). In addition intercalations of grainstones to rud-
stones appear. The calcareous dinocysts are scarce and repre-
sented  by  Stomiosphaerina  proxima  Rěhánek  (Fig. 5C,D).
The calpionellid association consists of the Crassicollaria and
Tintinnopsella  and  is  represented  by  Crassicollaria  colomi
Doben  (Fig. 5E),  Crassicollaria  parvula  Remane  (Fig. 5F),
Crassicollaria  massutiniana  (Colom)  (Fig. 5G),  Crassicol-
laria  brevis  Remane  (Fig. 5H),  Crassicollaria  intermedia
Durand-Delga  (Fig. 5I),  Tintinnopsella  remanei  (Borza)
(Fig. 5J), and small Tintinnopsella carpathica (Murgeanu &
Filipescu) (Fig. 5K). The Calpionella is scarce and recorded
only in the topmost part of the zone. The large forms such as
Calpionella  grandalpina  Nagy  and  Calpionella  elliptalpina
Nagy were not found.

This interval is characterized by the taphonomic and sedi-

mentary condensation. The evidence of this condensation is
expressed by the mixture of different subzones of Crassicol-
laria Zone and glauconitic grains. This condensation prevents
the subdivision of Crassicollaria Zone in the studied section.

The topmost part of this interval is marked by storm de-

posits characterized by grainstones of peloids and resedi-
mented shallow-water fossils similar to those illustrated in
Fig. 6 (A,B).

Early Berriasian

Calpionella Zone

Alpina Subzone (Samples RSV 23—38)

The acme of small spherical forms of Calpionella alpina

Lorenz (Fig. 6C—E) marks a change in the assemblage com-
position and defines the base of the Calpionella Zone, its Al-
pina Subzone (sensu Remane 1986; Lakova 1994; Olóriz et
al. 1995; Pop 1996; Reháková & Michalík 1997; Houša et al.
1999; Boughdiri et al. 2006; Andreini et al. 2007; Wimbledon
et al. 2011; Michalík & Reháková 2011 and others) (Fig. 9).
The lower part of this zone is recognized as coincident with
the Tithonian/Berriasian boundary.

Another change is the abrupt decrease in the abundance of

Crassicollaria. Only a few scarce Crassicollaria parvula
Remane cross the Jurassic/Cretaceous boundary.

Microfacies show an evident relationship of this subzone

with storm deposits. These deposits began in the Crassicol-
laria

Zone and are very frequent in the lower part of the

Calpionella Zone.

The presence of these storm deposits and the considerable

amounts of resedimented fossils in the Jurassic/Cretaceous
boundary interval may be a response to a sea-level fall dur-
ing this period, with the consequent influence of the shallower
water conditions.

Thus, the Jurassic/Cretaceous boundary is placed within

the sample number 23, about 6 meters above the base of the
El Americano Member (Fig. 9).

Ferasini Subzone (Samples RSV 38—51)

Upwards within the El Americano Member, the base of the

Ferasini Subzone is characterized by the First Occurrence
(FO) of Remaniella ferasini Catalano (Fig. 6F,G) (Pop 1994,
1996; Reháková & Michalík 1997) (Fig. 9). This biostrati-
graphic unit has also been referred to as the Remaniella Sub-
zone (Olóriz et al. 1995).

Remaniella is scarce and very poorly preserved in the facies

studied. Due to the absence of collars only a few specimens
were identified. Nonetheless, the shape of the lorica of many
specimens resembles the type of the remaniellids. Calpionella
alpina Lorenz is frequent and dominates the assemblage. Tin-
tinnopsella carpathica (Murgeanu & Filipescu) (Fig. 6H) is
also frequent; there are also scarce Crassicollaria parvula.

The microfacies of this interval are radiolarian and calpio-

nellid mudstones to wackestones. The matrix is microsparitic
and dolomitized in some parts and, as a consequence, the col-
lars of the Remaniella are persistently damaged (Fig. 6I).
Abundant spores of Globochaete alpina Lombard were ob-
served (Fig. 6J). Dark organic matter and pyrite are present
in all intervals.

Elliptica Subzone (Samples RSV 52—83)

The FO of Calpionella elliptica Cadish (Fig. 7A) defines

the base of the Elliptica Subzone (Catalano & Liguori 1971;
Reháková  &  Michalík  1997)  and  is  recognized  herein  to-
wards the top of the El Americano Member (Fig. 9). Calpio-
nella  alpina  Lorenz  still  dominates  over  other  species.
Tintinnopsella  carpathica  (Murgeanu  &  Filipescu)  is  abun-
dant but always subordinated to  Calpionella alpina Lorenz.
Remaniella is represented by two species: Remaniella ferasini
(Catalano)  (Fig. 6F,G)  and  Remaniella  duranddelgai  Pop
(Fig. 7B). The occurrence of calpionellids joined by the collar
(Fig. 7C,D) is very common in this level. This phenomenon
was described by Borza (1969) and Colom (1988) and inter-
preted as the form of calpionellid reproduction.

The microfacies of this interval are less variable compared

to the preceding. The rocks represent mudstones and wacke-
stones  with  radiolarians  and  calpionellids  and  abundant
Globochaete alpina Lombard, frequent incursions of resedi-
mented ostracods, pelecypod fragments and abundant biotur-
bation  (Fig. 7E).  The  rocks  commonly  contain  dark  organic
matter and the matrix is microsparitic as a rule. This type of
preservation  makes  calpionellids  hardly  determinable.  A  re-
duced number of specimens of Remaniella are preserved with
collars.  The  majority  of  specimens  are  with  damaged  or  no
collar. A frequent recrystallization of the lorica made it impos-
sible to distinguish between different species.

203

CALPIONELLID DISTRIBUTION AND MICROFACIES ACROSS JURASSIC/CRETACEOUS BOUNDARY (W CUBA)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

Late Berriasian

Calpionellopsis Zone (Samples RSV 84—141)

An important change in the calpionellid assemblage is

marked with the FO of the Calpionellopsis which defines the
base of the Calpionellopsis Zone. In the section studied, this
change takes place at the topmost part of the El Americano
Member, and the biozone spans into the whole overlying
Tumbadero Member (Fig. 9). The FO of the Calpionellopsis
which is normally represented by Calpionellopsis simplex
(Colom) (Fig. 7F) in the section studied is concurrent with the
appearance of Calpionellopsis oblonga (Cadish) (Fig. 7G).

Towards the top of the biozone, Calpionella alpina Lorenz

and Calpionella elliptica Cadish become scarce. On the other
hand, Tintinnopsella carpathica (Murgeanu & Filipescu) is
very common throughout, and the FO of Tintinnopsella longa
(Colom) (Fig. 7H) is in the middle part of the zone, and the
species is always scarce.

It is worth noting the appearance of many aberrant forms

within  this  interval  similar  to  those  reported  by  Reháková
(2000b)  for  the  Calpionellopsis  Zone  (Fig. 7I,J).  The  most
diversified calpionellid assemblage is recorded in this inter-
val,  and  is  represented  by  Tintinnopsella  subacuta  (Colom)
(Fig. 7K),  Tintinnopsella  longa  Colom  (Fig. 7H),  Tintinnop-
sella  carpathica  (Murgeanu  &  Filipescu)  (Fig. 5K),  Am-
phorellina  lanceolata  Colom  (Fig. 8A),  Calpionella  minuta
Houša (Fig. 8B), Lorenziella plicata  Le Hégarat & Remane
(Fig. 8C), Remaniella duranddelgai Pop (Fig. 7B), Remaniella
filipescui Pop (Fig. 8D) and Remaniella cadischiana (Colom)
(Fig. 8E).

In the course of the Calpionellopsis Zone, an interesting

radiolarian and sponges event occurs. The abundance of ra-
diolarians, sponges and organic matter increases consider-
ably. This event affects preservation of the calpionellids. The
radiolarian and sponges beds are much silicified, dolo-
mitized and the organic matter is oxidized (Fig. 8F,G). This
event may be attributable to upwelling currents.

Murgeanui Subzone (Sample RSV-141)

One specimen of Praecalpionellites murgeanui Pop

(Fig. 8H) was found in the upper part of this interval (sample
RSV-141). This index species indicates the presence of the
Murgeanui Subzone. No microfacies change is visible in this
horizon.

Early Valanginian

Calpionellites Zone, Darderi Subzone

(Samples RSV 142—145)

In an overlaying biomicrite limestone (wackestone) con-

taining rare calcified radiolarians and calpionellids, loricas
of Calpionellites darderi (Colom) (see Fig. 8I) were identi-
fied. This index marker characterizes the Early Valanginian
Darderi Subzone of the Calpionellites Zone.

Discussion

Detailed bed-by-bed sampling in the Rancho San Vicente

section of “Sierra de los Órganos” in western Cuba allows

the recognition of a precise calpionellids and facies distribu-
tion (Fig. 9).

Lower Tithonian shallow-water carbonated bank San Vi-

cente Member lacks biostratigraphical markers which makes
the definition of the stratigraphic range of facies very diffi-
cult. Thus, it was dated by superposition and partially by the
occurrence of the Early Tithonian Semiradiata Zone underly-
ing the Chitinoidella-bearing limestones. The facies of this
member are considered in the present work as representing a
shallow-water bank without terrigenous influence, but addi-
tional work is necessary to define more precisely the dynamics
of this carbonated bank. The topmost part of the San Vicente
Member is dated as Early Tithonian (Semiradiata Zone). In
previous works (Pszczółkowski 1978, 1999), the contact be-
tween the San Vicente and the El Americano Members was
dated as Kimmeridgian—Tithonian.

The age from Pszczółkowski (1978, 1999) is coincident

with  Goldhammer  &  Johnson’s  (2001)  second  order  trans-
gression  in  the  Kimmeridgian/Tithonian  in  the  whole  Gulf
of  Mexico  province  and  Proto-Caribbean.  Nonetheless,  in
more detailed work it is possible to find a diachronism in the
apparition  of  the  pelagic  conditions.  This  diachronism  re-
veals  that  the  San  Vicente  carbonated  bank  prevailed  for  a
time after the initiation of the global sea-level rise. The glo-
bal sea-level rise started in the Kimmeridgian/Tithonian and
the complete drowning of the San Vicente bank occurred in
the  Upper  Tithonian.  According  to  Rosales  et  al.  (1992)  an
anoxic  event  took  place  in  the  Kimmeridgian/Tithonian  in
the  Gulf  of  Mexico  marked  by  the  formation  of  facies  en-
riched  in  organic  matter.  However,  the  San  Vicente  section
does not show a clear anoxic facies. In contrast to the asser-
tions  by  Pszczółkowski  &  Myczyński  (2010),  the  presence
of only juvenile and the scarcity or lack of adult gastropods
are interpreted herein as rather due to taphonomic processes,
similar to the interpretations by Fernández-López & Meléndez
(1995),  than  as  a  consequence  of  low  oxygenation  levels.
The position of the San Vicente section in more oxygenated
waters is a reasonable explanation of a longer permanence of
the  carbonated  bank.  Nonetheless,  we  do  not  have  enough
evidence to reject the drowning of the San Vicente carbonate
bank as a result of sea-level rise and the action of the regional
anoxic event on the aforementioned drowning of the carbon-
ate platform.

The pelagic facies represented by the lower part of the

El Americano Member are mainly composed by Saccocoma-
bearing  limestones  with  clear  signals  of  sedimentary  and
taphonomic  condensation  (mixture  of  calpionellid  biozones
and  presence  of  glauconite).  Similar  Saccocoma  facies  al-
though  Kimmeridgian  in  age  were  described  by  Reháková
(2000b).  According  to  Matyszkiewicz  (1997)  and  Keupp  &
Matyszkiewicz (1997), the saccocomids were very abundant
in the late transgressive system tract and probably within the
high-stand  deposits  of  the  northern  Tethys  during  the  Late
Oxfordian/Early  Kimmeridgian  and  the  latest  Kimmerid-
gian/Early  Tithonian.  Saccocoma  is  recorded  in  the  United
States  (Brönnimann  1954),  Europe  (Pisera  &  Dzik  1979),
Mexico (Aguilera-Franco & Franco-Navarrete 1995), North-
ern  Africa  (Matyszkiewicz  1997),  Asia  (Hess  2002),  Cuba
(Brodacki 2006) and Argentina (Kietzmann & Palma 2009).

206

LÓPEZ-MARTÍNEZ, BARRAGÁN, REHÁKOVÁ and COBIELLA-REGUERA

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

In all those areas, these facies span from the Kimmeridgian
through to the Tithonian.

The recognition of this type of facies in Cuba is important

due  to  its  stratigraphical  coincidence  with  coeval  strata  from
Mexico and Argentina. In the three areas (Cuba, Mexico and
Argentina), this type of deposits started its record during ear-
liest Late Tithonian and may be the result of a connection be-
tween  the  Tethys  and  the  Pacific  Ocean  during  the  sea-level
rise. This fact is difficult to discern due to the absence of re-
ports of Saccocoma facies in other parts between Mexico and
Argentina, which may be due to the scarcity of works on the
topic in those areas. It is evident that the sea-level rise identi-
fied  here  within  the  Chitinoidella  Zone  could  be  correlated
with the same sea-level rise expressed by Reháková (2000b).

The Jurassic/Cretaceous boundary was easily identified be-

cause  of  the  dominance  of  Calpionella  alpina  Lorenz  in  the
assemblage  in  the  bed  number  RSV-23,  about  six  meters
above the base of the El Americano Member. Frequent storm
deposits in the top part of the Crassicollaria Zone closely re-
lated  to  the  Jurassic/Cretaceous  boundary  could  be  attribut-
able  to  a  response  to  a  global  sea-level  drop.  This  sea-level
drop may be correlated with the limit between third order cy-
cles 1.3 and 1.4 in the super cycle LZB1 of the Sea-level curve
sensu Haq et al. (1988).

It is worth mentioning that previous works (i.e.

Pszczółkowski & Myczyński 2010) interpreted the Jurassic-
Cretaceous transition as a long-term subsidence that masked
the global Tithonian/Berriasian sea-level drop in outcrops of
the area. Nonetheless, the abundance of shallow-water fos-
sils (gastropods, pelecypods), reworked materials and abun-
dant storm deposits across this boundary documented in the
present research, clearly reflect a sea-level drop after the sea-
level rise recorded in the Boneti Subzone and which drowned
the San Vicente carbonate bank.

Interesting bioevents occur in the transition between the

Elliptica Subzone and the Calpionellopsis Zone. This transi-
tion should be represented by the FO of the Calpionellopsis
simplex (Colom), however, the first specimens of the Calpio-
nellopsis in the section are identified as Calpionellopsis ob-
longa (Cadish).

The transition through Elliptica-Oblonga Subzones oc-

curred  without  an  apparent  sedimentary  break  in  the  section
and,  therefore,  it  is  difficult  to  associate  the  absence  of  the
Simplex  Subzone  to  a  sedimentary  gap.  To  assess  this  prob-
lem we considered two options. The first refers to the possi-
bility of a very thin Simplex Subzone, and as a consequence,
its loss by sampling effect. This explanation is hard to assume
due to the intensity of the sampling but there is a possibility to
consider a sedimentary condensation. The second assumption
is  a  possible  confusion  between  Calpionellopsis  simplex  and
Calpionellopsis oblonga, due to the bad preservation. This ex-
planation is hard to assume as well, due to the differences in
the morphology of the lorica between the two taxa, even in ob-
lique  sections  and  without  preserved  collars.  Remane  (1985)
explained  that  this  confusion  is  only  possible  in  the  D2—D3
passage where transitional forms occur. An appropriate expla-
nation of this phenomenon is out of the scope of the present
work, and perhaps a regional detailed composite section will be
necessary to unravel this biostratigraphic interval in the future.

Another important change in microfacies and fossil assem-

blage occurs in the Oblonga Subzone. Within this unit, radio-
larians and organic matter become very abundant (Fig. 8F,G).
The facies of this interval are darker and display frequent sili-
ceous nodules.

The increase of radiolarians and organic matter is attribut-

able in the present work to upwelling currents. This interpre-
tation is supported by the abundance of sponge spicules and
by the fact that all siliceous nodules found in the studied sec-
tion  were  diagenetic.  It  is  interesting  to  note  that  aberrant
calpionellids (Fig. 7I,J) are only present within this interval
of  the  radiolarian  facies.  There  may  be  a  relationship  be-
tween the nutrification associated with the upwelling system
and  these  aberrant  calpionellids,  but  more  detailed  work  is
necessary to prove this assertion.

Conclusion

The high resolution sampling of an outcrop of the Guasasa

Formation in the Rancho San Vicente section of the “Sierra de
los Órganos” provided new and well-supported data about fa-
cies  and  calpionellid  distribution  across  the  Jurassic/Creta-
ceous boundary in western Cuba. The drowning event of the
San Vicente carbonate bank, a major regional paleogeographic
element on the facies studied, occurred during the earliest Late
Tithonian, Boneti Subzone, and led to deposition of the pelagic
facies  of  the  El  Americano  Member.  Thus,  the  stratigraphic
contact between the San Vicente and the El Americano Mem-
bers, the two lowest units of the Guasasa Formation, is Early/
Late  Tithonian  and  not  Kimmeridgian/Tithonian  as  consid-
ered in previous works. The sea-level rise associated with this
drowning  event  was  probably  the  cause  of  the  dispersion  of
Saccocoma  sp.  into  different  paleogeographic  domains,  in-
cluding  the  Neuquen  Basin.  The  Jurassic/Cretaceous  bound-
ary  in  the  studied  section  is  identified  at  sample  number 23,
six meters above the contact between the San Vicente and the
El  Americano  Members  and  not  in  the  topmost  part  of  the
latter unit as previously assumed. The facies of this bound-
ary are linked to the global sea-level drop recognized for that
age, indicated in the facies of this study by a concomitant shal-
low-water influence and storm deposits. The top of the strati-
graphic section corresponds to the Early Valanginian Darderi
Subzone of the Calpionellites Zone. Finally, the distribution
of calpionellids through the section allows good correlation
of the Jurassic/Cretaceous Cuban facies with European sec-
tions of the same period. Even though small differences were
found between the two areas, they can be attributed to spe-
cial  local  sedimentary  conditions  such  as  condensation  and
to bad preservation of some specimens.

Acknowledgments: This research was possible due to the fi-
nancing of the Projects PAPIIT IN 108709 and IN 109912-3
from the Dirección General de Asuntos del Personal
Académico, Universidad Nacional Autónoma de México. The
research was also supported by the Grant Agencies for Sciences
of Slovakia (Project APVV 0644-10; VEGA 2/0068/11 and
VEGA 2/0042/12) and by the Project “Evolución geodinámica
(paleogeográfica) de Cuba occidental y central entre el Jurásico

207

CALPIONELLID DISTRIBUTION AND MICROFACIES ACROSS JURASSIC/CRETACEOUS BOUNDARY (W CUBA)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

Tardío y el Plioceno”, from the University of Pinar del Río,
Cuba. The paper is a contribution to the activity of the Berria-
sian Working Group of the international Subcomission on
Cretaceous Stratigraphy.

References

Aguilera-Franco N. & Franco-Navarrete S. 1995: Biochronostrati-

graphic importance and environmental implications of the ge-
nus Saccocoma arachnoidea (Brönnimann, 1955) in southeast
Mexico during the Middle Tithonian. Geol. Soc. Mexico Bull.
52, 3—4, 18—21 (in Spanish).

Altiner D. & Özkan S. 1991: Calpionellid zonation in north-western

Anatolia (Turkey) and calibration of the stratigraphic ranges of
some benthic foraminifers at the Jurassic-Cretaceous boundary.
Geol. Romana 27, 215—235.

Andreini G., Caracuel J.E. & Parisi G. 2007: Calpionellid bio-

stratigraphy of the Upper Tithonian—Upper Valanginian inter-
val in Western Sicily (Italy). Swiss. J. Geosci. 100, 179—198.

Bakalova D. 1977: La succession á Calpionelles de la coupe prés du

village de Ginci, Bulgarie du Nord-Ouest. C.R. Acad. Bulg.
Sci. 30, 423—426.

Borza K. 1969: Die Mikrofazies und Mikrofossilien des Oberjuras

un der Unterkreide der Klippenzone der Westkarpaten. Verlag
Slowak Acad. Wiss., Bratislava, 5—301.

Borza K. 1984: The Upper Jurassic—Lower Cretaceous parabiostrati-

graphic scale on the basis of Tintinninae, Cadosinidae, Stomio-
sphaeridae, Calcisphaerulidae and other microfossils from the
West Carpathians. Geol. Zbor. Geol. Carpath. 35, 539—550.

Boughdiri M., Sallouhi H., Maâlaoui K., Soussi M. & Cordey F.

2006: Calpionellid zonation of the Jurassic-Cretaceous transi-
tion in north Atlasic Tunisia. Updated Upper Jurassic stratigra-
phy of the “Tunisian Trough” and regional correlations. C.R.
Geosci. 338, 1250—1259.

Brodacki M. 2006: Functional anatomy and mode of life of the latest

Jurassic crinoid Saccocoma. Acta Paleont. Pol. 51, 261—270.

Brönnimann P. 1954: On the occurrence of calpionellids in Cuba.

Eclogae Geol. Helv. 46, 263—268.

Catalano R. & Liguori V. 1971: Facies and Calpionellids from

western Sicilia. In: Farinacci A. (Ed.): Proceedings of the II
Planktonic Conference, Roma, 1970. Tecnoscienza, Roma,
167—209 (in Italian).

Cobiella-Reguera J.L. 2008: Palinspastic reconstruction of the Me-

sozoic paleomargin from North America in western Cuba and
southeast of Gulf of Mexico. Implications for the evolution of
the southeast Gulf of Mexico. Rev. Mex. Cien. Geol. 25, 3,
382—401 (in Spanish).

Cobiella-Reguera J.L. & Olóriz F. 2009: Oxfordian—Berriasian

stratigraphy of the North American paleomargin in western
Cuba: Constraints for the geological history of the proto-Carib-
bean and the early Gulf of Mexico. In: Bartolini C. & Román
Ramos J.R. (Eds.): Petroleum systems in the southern Gulf of
Mexico. Amer. Assoc. Petrol. Geol. Mem. 90, 421—451.

Colom G. 1988: A revision of a Tintinnid group (Infusoria, Oligot-

richa, loricated). The evolution of their species in the Paleozoic
and secondary seas. Rev. Esp. Paleont. 3, 71—104 (in Spanish).

Fernández-Carmona J. 1998: Upper Jurassic—Lower Cretaceous

(Neocomian) biostratigraphy of western Cuba and its applica-
tion to the petroleum exploration. Ph.D. Thesis, CEINPET, La
Habana, 1—90 (in Spanish).

Fernández-López S. & Meléndez G. 1995: Taphonomic gradients in

Middle Jurassic ammonites of the Iberian Range (Spain). In:
Gayet M. & Courtinat B. (Eds.): First European Palaeontologi-
cal Congress, Lyon 1993. Geobios, M.S. 18, 155—165.

Furrazola-Bermúdez G. & Kreisel K. 1973: The fossil tintinnids of

Cuba. Rev. Tecnol. 11, 27—45 (in Spanish).

Goldhammer R.K. & Johnson C.A. 2001: Middle Jurassic—Upper

Cretaceous  paleogeographic  evolution  and  sequence-strati-
graphic  framework  of  the  Northwest  Gulf  of  Mexico  rim.  In:
Bartolini C., Buffler R.T. & Cantú-Chapa A. (Eds.): The west-
ern Gulf of Mexico Basin: Tectonics, sedimentary basins, and
petroleum  systems:  Tulsa,  Oklahoma,  E.U.A.  Amer.  Assoc.
Petrol. Geol. Mem. 79, 45—8.

Grandesso P. 1977: Tithonian pre-Calpionellids and their relations

with Rosso Ammonitico Veneto. [Gli strati a Precalpionellidi
del Titoniano e I loro raporti conil Rosso Ammonitico Veneto.]
Mem. Sci. Geol. 32, 1—15 (in Italian).

Haq B.U., Hardenbol J. & Vail P.R. 1988: Mesozoic and Cenozoic

chronostratigraphy and cycles of sea-level change. In: Wilgus
C.K., Hastings B.S., Kendall C.G.St.C., Posamentier H.W.,
Ross C.A. & van Wagoner J.C. (Eds.): Sea-level changes – an
integrated approach. Soc. Econ. Paleont. Miner. Spec. Publ.
42, 26—108.

Hatten C.W. 1967: Principal features of Cuban geology: discussion.

Amer. Assoc. Petrol. Geol. Bull. 51, 5, 780—789.

Herrera N.H. 1961: Contribution to the stratigraphy of the Pinar del

Río Province. Rev. Soc. Cubana Ing. 61, 22—44 (in Spanish).

Hess H. 2002: Remains of Saccocomids (Crinoidea: Echinodermata)

from the Upper Jurassic of southern Germany. Stuttgarter Beitr.
Naturkunde, Ser. B 329, 1—57.

Houša V., Krs M., Krsová M., Man O., Pruner P. & Venhodová D.

1999: High-resolution magnetostratigraphy and micropalaeon-
tology across the J/K boundary strata at Brodno near Žilina,
western Slovakia: Summary of results. Cretaceous Research
20, 699—717.

Iturralde-Vinent M. 1997: Introduction to the geology of Cuba. In:

Furrazola-Bermúdez G. & Nún

~ez-Cambra K. (Eds.): Studies

on the Geology of Cuba. Centro Nacional de Información
Geológica, La Habana, 35—68 (in Spanish).

Keupp H. & Matyszkiewicz J. 1997: Zur Faziesrelevanz von Sacco-

coma-Resten (Schwebcrinoiden) in Oberjura-Kalken des nördli-
chen Tethys-Schelfs. Geol. Blätter Nordost-Bayern 47, 53—70.

Khudoley K. & Meyerhoff A. 1971: Paleogeography and geological

history of Greater Antilles. Geol. Soc. Amer. Mem. 129, 1—199.

Kietzmann D. & Palma R. 2009: Saccocomid microcrinoids in the

Tithonian of the Neuquen Basin. An unexpected presence out-
side of the Tethyan region? Ameghiniana 46, 4, 695—700 (in
Spanish).

Kreisel K. & Furrazola-Bermúdez G. 1971: Preliminary notes

about the distribution of Tintinnids in Cuba. I.C.L. 5, 1—24
(in Spanish).

Lakova I. 1993: Middle Tithonian to Berriasian praecalpionellid

and calpionellids zonation of the Western Balkanides, Bulgaria.
Geol. Balcanica 23, 3—24.

Lakova I. 1994: Numerical criteria of precise delimitation of the

calpionellid Crassicollaria and Calpionella zones in relation to
the Jurassic/Cretaceous system boundary. Geol. Balcanica 24,
23—30.

Lugo E.J.E. 1975: Presence of Chitinoidella sp. (Tintinnidea, Codonel-

lidae) in the Jurassic of the Southeastern of Mexico. Bull. Assoc.
Mex. Geol. Petrol. 27, 10—12, 451—465 (in Spanish).

Matyszkiewicz J. 1997: Microfacies, sedimentation and some aspects

of diagenesis of Upper Jurassic sediments from elevated parts of
the Northern peri-Tethyan Shelf: a comparative study on the
Lochen area (Schwäbische Alb) and the Cracow area (Cracow-
Wieliun Upland, Poland). Ber. Geowiss. Abh. 21, 1—111.

Michalík J. & Reháková D. 2011: Possible markers of the Jurassic/

Cretaceous boundary in the Mediterranean Tethys: A review
and state of art. Geosci. Frontiers 2, 4, 475—490.

Moretti I., Tenreyro R., Linares E., Lopez J.G., Letouzey J., Magnier

208

LÓPEZ-MARTÍNEZ, BARRAGÁN, REHÁKOVÁ and COBIELLA-REGUERA

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 3, 195—208

C., Gaumet F., Lecomte J., Lopez J.O. & Zimine S. 2003: Pe-
troleum systems of the Cuban north-west offshore zone. In:
Bartolini C., Buffler R. & Blickwelde J. (Eds.): The circum-
Gulf of Mexico and the Caribbean. Hydrocarbon habitats, ba-
sin formation, and plate tectonics. Amer. Assoc. Petrol. Geol.
Mem. 79, 675—696.

Myczyński R. & Pszczółkowski A. 1990: Tithonian stratigraphy in

the Sierra de los Organos, Western Cuba: correlation of the am-
monite and microfossil zones. In: Pallini G., Cecca F., Cresta S.
& Sanantonio M. (Eds.): Fossili, Evoluzione, Ambiente. Atti del
secondo convegno internazionale, Pergola 25—30 ottobre 1987,
405—415.

Olóriz F., Caracuel J.E., Marques B. & Rodríguez-Tovar F.J. 1995:

Assemblages of tintinnoids on ammonitico rosso facies from
the Sierra Norte (Mallorca). Rev. Espan

~ola Paleont. Spec. Issue

in honor to Dr. Guillermo Colom, 77—93 (in Spanish).

Piotrowska K. 1978: Nappe structures in the Sierra de los Organos,

western Cuba. Acta Geol. Pol. 28, 1, 97—170.

Pisera A. & Dzik J. 1979: Tithonian crinoids from Rogoznik (Pieniny

Klippen Belt, Poland) and their evolutionary relationships.
Eclogae Geol. Helv. 72, 805—849.

Pop G. 1976: Tithonian—Valanginian calpionellid zones from Cuba.

D.S. edin ., Inst. Geol. Geofiz. (3. Paleontologie), 62, 237—266.

Pop G. 1994: Calpionellid evolutive events and their use in bio-

stratigraphy. Romanian J. Stratigr. 76, 7—24.

Pop G. 1996: Trois nouvelles espéces du genre Remaniella (Calpio-

nellidae Bonet, 1956). C.R. Acad. Sci. Paris 332, 2a, 317—323.

Pszczółkowski A. 1978: Geosynclinal sequences of the Cordillera de

Guaniguanico in western Cuba; their lithostratigraphy, facies de-
velopment, and paleogeography. Acta Geol. Pol. 28, 1—96.

Pszczółkowski A. 1994: Lithostratigraphy of Mesozoic and Paleo-

gene rocks of Sierra del Rosario, western Cuba. Studia Geol.
Pol. 105, 39—66.

Pszczółkowski A. 1999: The exposed passive margin of North Ame-

rica in western Cuba. In: Mann P. (Ed.): Caribbean basins, sedi-
mentary basins of the World, 4. Elsevier, Amsterdam, 93—121.

Pszczółkowski A. & Myczyński R. 2003: Stratigraphic constraints

on  the  Late  Jurassic—Cretaceous  paleotectonic  interpretations
of  the  Placetas  belt  in  Cuba.  In:  Bartolini  C.,  Buffler  R.T.  &
Blickwede  J.F.  (Eds.):  The  Circum-Gulf  of  Mexico  and  the

Caribbean: Hydrocarbon habitats, basin formation, and plate-
tectonics. Amer. Assoc. Petrol. Geol. Mem. 79, 545—581.

Pszczółkowski A. & Myczyński R. 2010: Tithonian—Early Valang-

inian evolution of deposition along the proto-Caribbean margin
of North America recorded in Guaniguanico successions
(western Cuba). J.S. Amer. Earth Sci. 29, 225—253.

Pszczółkowski A., García-Delgado D. & Gil González S. 2005: Calpio-

nellid and nannoconid stratigraphy and microfacies of limestones
at the Tithonian—Berriasian boundary in the Sierra del Infierno
(western Cuba). Ann. Soc. Geol. Pol. 75, 1—16.

Reháková D. 2000a: Evolution and distribution of the Late Jurassic

and Early Cretaceous calcareous dinoflagellates recorded in
the Western Carpathian pelagic carbonate facies. Miner. Slovaca
32, 79—88.

Reháková D. 2000b: Calcareous dinoflagellate and calpionellid bio-

events versus sea-level fluctuations recorded in the West-Car-
pathian (Late Jurassic/Early Cretaceous) pelagic environments.
Geol. Carpathica 51, 4, 229—243.

Reháková D. 2002: Chitinoidella Trejo, 1975 in Middle Tithonian

carbonate pelagic sequences of the West Carpathian Tethyan
Area. Geol. Carpathica 53, 6, 369—379.

Reháková D. & Michalík J. 1997: Evolution and distribution of calpio-

nellids–the most characteristic constituents of Lower Cretaceous
Tethyan microplankton. Cretaceous Research 18, 493—504.

Remane J. 1985: Calpionellids. In: Bolli H., Saunders J.B. & Perch-

Nielsen K. (Eds.): Plankton stratigraphy. Cambridge University
Press, Cambridge, 555—572.

Rosales E., Bello-Montoya R. & Philp R.P. 1992: Petroleum

geochemistry of Jurassic and Cretaceous rocks in western Sierra
de Chiapas. Southern Mexico. Acta Earth Sci. Fac., Autonomous
University of Nuevo León 7, 65—69.

Saura E., Vergés J., Brown D., Lukito P., Soriano S., Torrescusa S.,

García R., Sánchez J.R., Sosa C. & Tenreyro R. 2008: Struc-
tural and tectonic evolutions of western Cuba fold and thrust
belt. Tectonics 27, TC4002, doi:10.1029/2007TC002237

Wimbledon W.A.P., Casellato C.E., Reháková D., Bulot L.G., Erba

E., Gardin S., Verreussel R.M.C.H., Munsterman D.K. & Hunt
C.O. 2011: Fixing a basal Berriasian and Jurassic-Cretaceous
(J-K) boundary – is there perhaps some light at the end of the
tunnel? Riv. Ital. Paleont. Stratigr. 117, 2, 295—307.