UTRECHT MICROPALEONTOLOGICAL BUllETINS

UTRECHT
MICROPALEONTOLOGICAL
BUllETINS
IU S
UNES 0
I
QUANTITATIVE FORAMINIFERAL ANALYSIS AND
ENVIRONMENTAL INTERPRETATION OF THE PLIOCENE AND
TOPMOST MIOCENE ON THE SOUTH COAST OF SICILY
18

Editor C. W. Drooger
Department of Stratigraphy and Paleontology
State University of Utrecht
Oude Gracht 320, Utrecht, Netherlands
Bull. 1. T. FREUDENTHAL - Stratigraphy of Neogene deposits in the Khania
Province, Crete, with special reference to foraminifera of the family Plan orbulinidae
and the genus Heterostegina. 208 p., 15 pl., 33 figs. (1969) f32,-
Bull. 2. J. E. MEULENKAMP - Stratigraphy of Neogene deposits in the Rethymnon
Province, Crete, with special reference to the phylogeny of uniserial
Uvigerina from the Mediterranean region. 172 p., 6 pI, 53 figs. (1969)f 29,-
Bull. 3. J. G. VERDENIUS - Neogene stratigraphy of the Western Gualdalquivir
basin, S. Spain. 109 p., 9 pl., 12 figs. (1970) f28,-
Bull. 4. R. C. TJALSMA - Stratigraphy and foraminifera of the Neogene of the
Eastern Guadalquivir basin, S. Spain. 161 p., 16 pl., 28 figs (1971) f 44,-
Bull. 5. C. W. DROOGER, P. MARKS,/A. PAPP et al. - Smaller radiate Nummulites
of northwestern Europe. 137 p., 5 pl., 50 figs. (1971) f 37,-
Bull. 6. W. SISSINGH - Late Cenozoic Ostracoda of the South Aegean Island arc.
187 p., 12 pl., 44 figs. (1972) f57,-
Bull. 7. author's edition. F. M. GRADSTEIN - Mediterranean Pliocene Globorotalia,
a biometrical approach. 128 p., 8 pl., 44 figs. (1974) f 39,-
Bull. 8. J. A. BROEKMAN - Sedimentation and paleoecology of Pliocene lagoonalshallow
marine deposits on the island of Rhodos (Greece). 148 p., 7 pl.,
9 figs. (1974) f47,-
Bull. 9. D. S. N. RAJU - Study of Indian Miogypsinidae. 148 p., 8 pl., 39 figs.
(1974) f38,-
Bull. 10. W. A. VAN WAMEL - Conodont biostratigraphy of the Upper Cambrian
and Lower Ordovician of north-western bland, south-eastern Sweden.
128 p., 8 pl., 25 figs. (1974) f 40,-
Bull. 11. W. J. ZACHARIASSE - Planktonic foraminiferal biostratigraphy of the
Late Neogene of Crete (Greece). 171 p., 17 pl., 23 figs. (1975) f52,-

QUANTITATIVE FORAMINIFERAL ANALYSIS AND
ENVIRONMENTAL INTERPRETATION OF THE PLIOCENE AND
TOPMOST MIOCENE ON THE SOUTH COAST OF SICILY

Page
Preface . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5
Abstract . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 7
Chapter I. Introduction. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9
Purpose of investigation . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9
The formations. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 11
Methods of investigation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 12
Wash residues . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 13
Acknowledgements. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 14
Chapter II. Arenazzolo . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 17
Chapter III. Transitional interval. . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 21
Lithology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 21
The foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 23
. Conclusions. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 25
Chapter IV. Trubi . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 27
Lithology '. . . . . . . . . . . .. 27
Section 3. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 29
Section 4. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 34
Section Punta Piccola. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 36
Discussion of the lithology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 36
The foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 40
Preservation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 40
Benthonic foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 40
BIP ratio . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 40
Details of the eight meter "Accuracy" section . . . . . . . . . . . . .. 43
Species diversity. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 44
Distribution of species. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 48
Planktonic foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 56
Species diversity. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 56
Distribution of species , 57
Paleobathymetric estimates. . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 63
Biostratigraphic position Capo Rossello section . . . . . . . . . . . . . . . .. 72
Chapter V. Monte Narbone formation. . . . . . . . . . . . . . . . . . . . . . . . . .. 77
Lithology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 77
Discussion of the lithology . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 83

The foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 86
Preservation. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 86
Benthonic foraminifera " 86
B/P ratio. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 86
Species diversity. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 87
Distribution of species. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 91
Planktonic foraminifera. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 97
Species diversity , 97
Distribution of species , 98
Paleobathymetric estimates. . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 105
Biostratigraphic position Punta Piccola section. . . . . . . . . . . . . . . . .. 107
Chapter VI. Synthesis. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 111
Benthonic foraminiferal associations throughout the South Sicilian
Pliocene. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 111
Arenazzolo . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 115
Trubi. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 117
Monte Narbone formation. . . . . . . . . . . . . . . . . . . . . . . . . .. . . . . . .. 122
Chapter VII. The salinity crisis. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 125
Chapter VIII. Taxonomic notes. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 129
Numbered literature referring to bathymetric range charts. . . . . . . . . .. 135
References cited in the text. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 139
50 figures, 8 plates

This investigation was originally intended to aim at an environmental
interpretation of the Pliocene deposits in southern Sicily on the basis of
sedimentary and foraminiferal data. The sections investigated were assumed
to contain the "deepest" sediments of Early Pliocene age exposed on land
in the Mediterranean area.
The subject turned out to link with the work being done by international
teams which are trying to unravel the history of the Messinian salinity crisis
in the Mediterranean; part of these efforts comes under the current I.G .C.P.
project no. 96.
During the re~,earch period 1972-77 growing emphasis was put on the
quantitative aspect of the investigation, and a small part of one of the Sicilian
sections was chosen for a detailed analysis of counting methods and
techniques; the latter formed part of the I.G.C.P. project no. 1. Some of the
results of this methodological research, published by Zachariasse et al. in
U.M.B. 17, have been applied to arrive at the various conclusions to be
found throughout the present volume. The relevant parts of the methodological
chapters can be easily found in bulletin 17, but no special reference
is made to them in the present text.
For the final version of this volume the author has adhered to a line of
reasoning which fits in with the original purpose of his investigation. Accordingly,
the beginning and the end of the text refer to the Messinian
salinity crisis, but the main part in between deals with environmental assumptions
for the Cattolica basin Pliocene, where repetitive upwelling and
volcanic emanations seem to have played an important role in determining
the composition of faunas and sediments.

Benthonic and planktonic foraminiferal faunas have been investigated
quantitatively from sediments of the Pliocene and topmost Miocene on the
south coast of Sicily. Environmental and bathymetrical reconstructions
have been established on the basis of the lithological and foraminiferal
data.
Two sections are studied in detail: the Lower Pliocene Trubi formation
at Capo Rossello and the Middle and Upper Pliocene Monte Narbone formation
at Punta Piccola. In both sections relations between benthonic and
planktonic foraminiferal assemblages and lithology can be clearly established.
Continuous marine sedimentation occurred across the ill-defined Miocene-
Pliocene boundary, initially at depths of 50-100 m, but gradually the depth
increased to 500-800 m for the middle part of the Trubi. At the onset of
more clayey sedimentation at the base of the Narbone formation, depth of
deposition decreased to some 100-400 m.
For the relatively short biostratigraphic interval of the lower part of the
G. puncticulata Interval-Zone the paleobathymetry was estimated at three
localities revealing different depositional depths of the same type of Trubi
sediment. A multi-depressional paleogeography for the entire Mediterranean
during at least Late Messinian and Early Pliocene times is proposed to explain
the seemingly conflicting implications of both the "desiccated, deep
basin model" and the "shallow water, shallow basin model". This alternative
model involves syn- and post-Messinian subsidence and may easily account
for the presence of Trubi in deep basinal settings and elevated land-sections.
The sections on the south coast of Sicily seem to have been located in an
intermediate paleogeographical realm, i.e. on the slope from shoals to deeps.
Periods of upwelling are thought to be responsible for increased quantities
of planktonic foraminifera, diatoms and radiolarians in some laminated
intervals within the Trubi formation. Oxygen depletion at the bottom may
explain the low diversity and dwarfing of the benthonic foraminiferal
associations in these laminated sediments.
Precipitation of ferromanganese oxides during deposition of the Narbone
formation determined the composition of foraminiferal assemblages. Oligotypical
buliminidjbolivinid assemblages characterize the darker coloured,
ferromanganese-rich intervals, whereas Globorotalia bononiensis dominates
the planktonic associations in some of these horizons.
Deposition of the Monte Narbone formation progressed in a shallowing
environment. Superimposed on this process decreasing water temperatures
are recorded in the Upper Pliocene Globorotalia inflata Assemblage Zone.
7

More detailed information concerning the history of the Mediterranean
immediately after the Messinian salinity crisis, some 5 m. y. ago, is expected
to lead to a better understanding of the Mediterranean paleogeography in
Late Miocene times. Since Messinian paleogeography received new attention
through D.S.D.P. leg 13, it was made a central theme in the activities of the
International Geodynamics Programme of Working Group 3, resulting in the
symposium of Utrecht (Geodyn. Sci. Rep. 7, 1973), and subsequently it
became an essential part of I.G.C.P. Project 96 under the leadership of M.B.
Cita. During the last five years, a tremendous amount of data has been
gathered, more or less well digested, and some rather conflicting models of
the Mediterranean Messinian salinity crisis have been presented.
With respect to the two widely discussed models, the "desiccated, deep
basin model" (Hsii, Cita and Ryan, 1973) and the "shallow water, shallow
basin model" (e.g. Ogniben, 1957; Nesteroff, 1973), a better understanding
of the paleoenvironment in which the Early Pliocene sediments were deposited
has become of crucial importance. A realistic estimate of the depth
of deposition of these sediments together with the details of their contact
with the underlying Messinian are thought to yield conclusive arguments for
either one or the other model. A great depth of deposition (in the order of
magnitude of 2000 m and more) in combination with either an unconformable
or a sharp lower contact of these first normal-marine Pliocene sediments
are claimed to be strong evidence for the first model (cf. Cita, 1973). A
shallow depth of deposition and a normal stratigraphic contact would favour
the second model (cf. Nesteroff, 1973).
It should be emphasized that alternative theories do exist. Avoiding a
choice between deep and shallow, it has been postulated that desiccation was
a less wide-spread and repeated phenomenon; the Mediterranean might have
been replenished by the Atlantic waters throughout the Messinian (Selli,
1973; Drooger, 1975). In order to explain the different Messinian sequences,
the multidepressional or multi-de ad-sea model was proposed (Marks, in
Drooger,1973).
Within the scope of I.G.C.P. Project 96 valuable evidence for deep basins

and considerable lowering of the erosion basis has been presented for some
areas, such as the Gulf of Lion, the Po basin and the Levantine basin (Seminar
Gargnano, 1976), but for other areas such as the basins in Eastern
Spain and Crete, deep basin desiccation remains hard to reconcile with the
field data.
The lack of detailed paleoecologic investigations across and above the
boundary, based on quantitative methods instead of qualitative observations,
is painfully felt. The present study is an attempt to furnish detailed lithological
descriptions and numerical data on benthonic and planktonic foraminiferal
assemblages of closely sampled sections covering the Miocene-
Pliocene boundary interval as well as the major part of the Pliocene interval
on the southern coast of Sicily. These sections west of Porto Empedocle
were selected because they are situated near the axis of the Cattolica basin.
They are reputed to show the deepest water Lower Pliocene, exposed on
land, that can be found in and around the Mediterranean. This Lower
Pliocene would be comparable in depth of deposition with the contemporaneous
strata, cored in some of the sites in the centres of the deep Mediterranean
basins of today (Cita, 1973; 197 Sa).
In addition to the raw data we shall give an interpretation of the paleoecologic
history reflected in these sediments. Finally paleogeographic conclusions
will be drawn which may explain some of the controversial aspects
of the Messinian events in this part of the Mediterranean.
In 1972 the investigation started with an inspection of the lithology and
faunal distribution across the Miocene-pliocene boundary at Capo Rossello
and Eraclea Minoa. Four sections were closely sampled and the benthonic
as well as the planktonic foraminiferal faunas were studied quantitatively,
resulting in more or less representative distribution charts. The first results
were published (Brolsma, 197 Sa and b), the general conclusions of which are
the following.
Two widely used markers for the Lower Pliocene, Globorotalia margaritae
and G. puncticulata were found to be present, in small but unmistakable
numbers, from 12 m below the Miocene-pliocene boundary upwards at both
localities, amongst which the newly designated Miocene-pliocene boundary
stratotype (Cita, 197 Sa). This led us to question the correlation value of this
boundary stratotype and the suitability of both planktonic taxa as markers
for the Pliocene. The Miocene-pliocene boundary appeared to be situated
in a 0.50 m transitional interval. Primary unconformable contacts (Cita,
1973) were considered unlikely. The changes in benthonic as well as planktonic
foraminiferal assemblages across this interval appeared to be grada-

tional. Most Pliocene taxa, frequently considered to be newly introduced
from the Atlantic (Cita, 1973), are already present below this boundary in
similar proportions. This led us to doubt the assumed complete sterilization
of the Mediterranean at the end of the salinity crisis, i.e. at the end of the
Messinian (Cita, 1973, 1976). No indications of a catastrophic influx of
Atlantic waters, as proposed in the "desiccated, deep basin model" (Hsii,
Cita and Ryan, 1973), were observed either. The great depth of deposition
assumed for the first Pliocene sediments of these sections (cf. Cita, 197Sa)
could not be recognized from our data. The sediments directly underlying
the boundary were deposited at depths not exceeding wave-base, and the
gradational character of the boundary interval, in lithological as well as
faunal sense, revealed the gradual change to deeper environments which
ultimately, i.e. several meters above the boundary, might have resulted in
deposition in excess of 200 m. A gradual rise of sea-level and/or a moderate
rate of subsidence of the bottom, or both together seem to have been the
mechanisms which best explained our newly gathered data (Brolsma, 1975b).
These results were questioned during the Erice seminar (1975) of the
I.G.C.P.. Project 96. Re-arrangement of the earlier arguments and some new
data will be presented in the chapter on the Transitional interval.
More information concerning the history of the Pliocene Mediterranean
during a longer time-span would inevitably shed more light on the process
of return to normal marine 'conditions after the salinity crisis. With this in
mind, Lower to Upper Pliocene sediments at Capo Rossello and in a nearby
section called Punta Piccola were closely studied and sampled in detail. From
all samples, the benthonic and planktonic foraminiferal faunas were again
studied in a quantitative way. The results of this extended study will be
given in the following chapters.
In the meantime an 8 meter part of one of the sections at Capo Rossello
was selected for a pilot study on quantitative faunal methods within the
scope of I.G.C.P. Project 1, "Accuracy in time" (Utrecht Micropal. Bull.,
17). The results of this study, pertinent to our own investigation, are incorporated
in the present volume.
The sediments deposited during the latest part of the Messinian and early
middle parts of the Pliocene in southern Sicily can be divided into three
informal formations (see also Marchetti, 1957, 1960). In stratigraphic order
from bottom to top these are:
Arenazzolo - Grey to black coloured sediments directly overlying the

topmost Messinian evaporites, characterized by an irregular vertical as well
as horizontal alternation of fine to medium-grained sand and silty-sandy
clays. The unit has a variable thickness of 1 to 40 m (Ogniben, 1957), and
it is especially known from the Cattolica basin. It is the topmost unit of
the Messinian, because it is immediately underlying the Miocene-Pliocene
boundary stratotype at Capo Rossello (Cita, 1975a).
Trubi - Biogenic cream coloured limestones and marls mainly consisting of
calcareous nannofossils and foraminifera and attaining a thickness of
100 m or slightly more. Along Sicily's southern coast the unit is commonly
outcropping in cliffs of 40 m height.
Transitional strata between Arenazzolo and Trubi often show the contact
between these two units to be situated in gradational lithological sequences
of about 0.50 m, but at many places post-depositional gravityinduced
sliding and slumping simulates an unconformable contact (Brolsma,1975b).
Monte Narbone - Grey coloured marls characterized in their lower part by
brown horizons, which locally contain high concentrations of ferromanganese
oxides. This unit may attain a thickness of more than 150 m, but
a continuous section covering the entire sequence has not been found. At
Lido Rossello near Realmonte a composite section can be constructed,
extending upward into the Pleistocene.
The Arenazzolo has been studied at various localities in combination with
the lower few meters of the overlying Trubi formation (Brolsma, 1975). A
short review and some new arguments will be presented below. The transitional
strata between Arenazzolo and Trubi, re-sampled in a recently discovered
outcrop along the cliffs of Eraclea Minoa, will also be described and
discussed. The main subject of this paper is a more complete description of
the Trubi and the overlying marls.
"Quarternary Zero" soap was used to clean the Trubi faunas by boiling
the samples for one hour in soap and water. Each sample was washed over a
set of three sieves (600, 250 and 125 p). An Otto microsplitter was used to
reduce the combined residues to workable proportions. The scarcity of benthonic
foraminifera prevented the selection of the statistically more favourable
number of 300 specimens per sample and instead 100, 150 or 200
specimens were counted. Some samples proved to be too poor to furnish
even 100, especially those from the laminated and finely bedded intervals

and from some more indurated levels in the lower and uppermost parts of
the Capo Rossello section. The benthonic fauna increases in abundance in
the overlying Narbone unit in which only two samples proved to be very
poor. 300 planktonic specimens per sample could be obtained without any
difficulty.
For printing purposes related species are shown in combination in the
distribution charts, whereas various scattered and less frequent species have
been combined under the heading "Miscellaneous".
Plankton/benthos ratios have been estimated for all samples. In order to
speed up the investigation all benthonic forms per 200 counted planktonic
specimens were counted. Since this ratio is less reliable it will only be used
as a relative measure within these sections. It is called the B/P ratio.
For both the benthonic and planktonic faunas the number of species
per sample is plotted in figs. 7 and 8. Since the total numbers of counted
benthonic specimens per sample are not equal in all sections, the Fisher Q-
index (Fisher et al., 1943) was calculated for a ready comparison of the
samples. The value Q = 5 has previously been regarded as separating open
marine environments from restricted, nearshore marine environments (Murray,
1973, fig. 101); it proves to be an unlikely generalization if applied to
our sections.
WASH-RESIDUES
In addition to the benthonic and planktonic foraminiferal constituents,
other faunal and floral remains and anorganic components are present in
the wash-residues. Biogenic remains include: ostracod valves, pelecypod and
gastropod fragments, fish-teeth, echinoid spines and operculae. One pteropod
specimen has been recorded in sample PP 42 and has been identified
as Cavolinia (pers. comm. L. M. J. U. van Straaten). Radiolarians and diatoms
occur in large quantities in silica-rich intervals (W. R. Riedel and
A. Sanfilippo, and H. J. Schrader and R. Gersonde, Utrecht Micropal.
Bull. 17).
Spherical objects, a smaller and a larger type, are quite frequent, especially
in the laminated and ferromanganese-rich interbeds from the Capo Rossello
and Punta Piccola sections, respectively. These forms have tentatively been
identified by G. T. Boalch (Plymouth) as possible representatives of the
genus Pachysphaera (division Chlorophyta, class Prasinophyceae; cf. Boalch
and Parke, 1971, pl. 1, figs. 2 and 3, and our pl. 5, figs. la-c). M. Muir
(London) was doubtful whether these same specimens belonged to Halosphaera,
which is another group in the Prasinophyceae and is recorded in the

literature together with Pachysphaera from comparable marine environments.
These phytoplanktonic forms become saucer-shaped under compression,
whilst in water they may regain their spherical shape after being
dented with a needle, because the membrane shows considerable elasticity
(Wall, 1962, p. 356). These observations correspond very well with the two
types in our material. Recent representatives of these green algae have been
reported in surface waters but they are more abundant at a depth of 10 m
and probably also occur at greater depths in marine waters (op. cit., p. 360).
Tiny, sometimes bifurcating burrows appear to be quite numerous in
the residues of some of the samples. The bifurcating types may belong to
Chondrites. A rigid pyritic core is responsible for their preservations.
Brown, grey and cream coloured limestone grains are observed in most
of the samples, as well as small pyritic grains which in sample PP 42 show a
sulphurous coating. Occasional crystals of pyrite may also be present.
Quartz grains, cemented to small globular bodies, are present in some of the
samples but they are found as single grains as well (CR 95). Gypsum is
present as vitreous crystal fragments, as worn opaque grains, or as small
rosettes on limestone grains. Sulphurous material coats the gypsum fragments
in sample PP 49. Brown coloured, insoluble (in 10% HCL) grains
(ferromanganese-oxides?) occur in some of the samples from the dark sediments
of the Narbone formation. Siltstone fragments occur in one sample
(PP 49). The relative quantity of anorganic material such as sand, silt and
schist fragments increases significantly in the residues in the upper part of
the Punta Picola section, reaching a peak value in PP 49.
I am greatly indebted to C. W. Drooger for suggesting the research topic.
His encouragement and helpful criticism throughout the course of this
investigation in the field as well as in the laboratory, is gratefully acknowledged.
Thanks are extended to R. D. Schuiling and C. H. van der Weijden
who kindly examined some of the samples on their mineral content. For
the assistance in the field and stimulating discussions I am very grateful to
J. E. Meulenkamp, R. C. Tjalsma and J. A. Broekman. I wish to thank
W. J. Zachariasse for introducing me into the field of study of planktonic
foraminifera. I like to express my thanks to P. Marks, W. J. Zachariasse and
R. R. Schmidt for many suggestions and discussions, and to my roommates
Th. E. Wong, J. Hageman and A. A. H. Wonders for their friendship and
endurance while listening to my counting work and Messinian monologues.
I express my gratitude to J. Hofker (The Hague), W. H. Zagwijn (Haarlem),

c. Cadee (Texel), I. den Hartog-Adams (Beek), G. T. Boalch (Plymouth)
and M. Muir (London) who examined Pachysphaera material. I thank P. D.
Brolsma and M. Schone for their assistance and company in the field.
The careful drawings of the benthonic foraminifera and the Scan photographs
were made by J. P. van der Linden. The drawing of the textfigures
were made by P. Hoonhout, A. van Doorn and J. P. van der Linden. The
photographs in the text were printed by A. van Doorn and F. H. Henzen.
G. van 't veld prepared most of the samples. S. Schut typed many of the
distribution charts and M. Schone took care of the typing of the manuscript.
I thank them all for their efficient and careful work.

Data and conclusions from the earlier papers (Brolsma, 197 Sa, b) on the
Arenazzolo and overlying Transitional interval at Capo Rossello (fig. 1) and
Eraclea Minoa (fig. 2) will not be exhaustively repeated. During the seminar
in Erice (1975) the marine environment in which the Arenazzolo was deposited
was doubted by some of those present. The question was raised
whether the faunas described by Brolsma (1975) represented reworked
Tortonian faunas, incorporated in lacustrine sediments. In the latter case
one might expect: 1) a rather haphazard distribution of various species in
the Arenazzolo sediments, 2) a concentration of such forms in strata suggesting
considerable turbulence and supply of coarser sediment, and 3) a
drastic change in the quantitative distribution of all species at the transition
to the overlying Trubi.
1) Samples JT 1386-1388 of section 1 at Capo Rossello (op. cit., 1975b,
fig. 5) contain oligotypic assemblages in which Ammonia beccarii forms as
much as 75 and 90% of the fauna in samples 1387 and 1386, respectively.
Cribrononion excavatum makes up 20% of the fauna in the former sample.
Sample CR 6 is almost devoid of benthonic foraminifera but it does contain
abundant ostracode carapaces of Cyprideis pannonica var. agrigentina. At
Eraclea Minoa 80% of the fauna of sample 14 (fig. 2, section 1) is formed
by Rosalina globularis. The presence of such assemblages of very low diversity
cannot be reconciled with a derivation from older deposits, but it might
fit in with the assumption of restricted marine to lacustrine deposits.
2) Brolsma (1975) described small scale cross-lamination and sub-horizontal
parallel lamination in the sandier strata of the Arenazzolo at Capo Rossel-
10. According to J. A. Broekman (pers. comm.) the horizontally stratified
sands which sometimes show an upper part with small scale cross stratification,
are very similar to the "storm-stand" layers described by Reineck and
Singh (1971; see also our fig. 3). Such sands are regarded to be the result
of deposition from suspension-clouds, the material of which was taken up in
shallow water during storms. One of these storm layers and the directly
underlying and overlying clayey sediments were sampled. The sand-bed is
horizontally laminated and attains a thickness of 2 cm. Its position is 3.5 m
below the Arenazzolo/Trubi contact in an exposure some 200 m SE of the
proposed Miocene/pliocene boundary stratotype (Cita, 197 Sa). Sample

Fig. 3 Subhorizontally stratified and cross-laminated sandy interbeds in clayey Arenazzolo sediments
at Capo Rossello.
CRM 2 was taken from the storm-sand layer about 3 em above CRM 1 and 3
em below CRM 3. The latter two samples are from the adjoining clayey
sediments (fig. 4).
Accepting a storm-induced origin of the sandy strata we might expect
higher numbers of supposedly reworked forms in sample CRM 2. The number
of species per 150 specimens met with in the sand (48) is somewhat
lower than the numbers collected from the clays (56 and 60). The quantitative
composition of the faunas does not differ significantly, and there is no
clear evidence for a difference in addition of reworked specimens (cf. fig. 4).
Moreover, the assemblages make sense from an ecological point of view
(Brolsma, 197 5b).
3) The numerical variation of most planktonic taxa across the Transitional
interval is very small. It is hard to imagine that the faunas below the
Miocene-pliocene boundary were reworked and those above the boundary
were autochthonous. This would mean that after 2 million years, the newly
introduced Atlantic fauna would still contain the various species in the same
proportions.
In addition to these faunistic considerations some lithostratigraphic data
are not in accordance with a fresh-water origin of the entire Arenazzolo.
Ogniben (1957) described the Arenazzolo from Sicily as a formation of
variable thickness and best developed in synclinal areas. In anticlinal regions
the Trubi directly overlies either the "calcare di base" of the Messinian or

2 3
Ammonia beccarii
Bolivina dentellata-dilatata-spathulata
Bolivina scalprata var. miocenica
Bolivina spp.
Bulimina aculeata
Bulimina elongata var. subulata
Bulimina spp.
Cibicides lobatulus
Cibicides (pseudo )ungerianus
Cibicides refulgens
Cibicides spp.
Discorbis spp.
Elphidium spp.
Globocassidulina subglobosa
Gyroidina umbonata
Hanzawaia boueana
Hopkinsina bononiensis
Lenticulina spp.
Nonion spp.
Gridorsalis stellatus
Rosalina globularis
Reussella spinulosa
Uvigerina spp.
Golina hexagona
Pullenia spp.
Siphonina brady ana
Stilostomella adolphina
Miscellaneous
Indeterminable
Total number of counted specimens
Total number of counted species
20 15
15 11
1 4
3 9
8 8
3 2
4 2
1 4
25 19
8 1
2 5
4 1
4 4
2 3
5 6
1 1
4 4
1 4
1 1
4 4
1 1
6 6
2 1
3 3
4 3
1 3
12 19
5 6
150 150
48 60
Distribution chart of the benthonic species from the storm-sand layer and adjoining clayey
sediments in the Arenazzolo at Capo Rossello.
the Tortonian sediments, whereas the synclines show the succession: evaporites-Arenazzolo-Trubi.
Petrographically the Arenazzolo was classified as
an arkosic calcarenite, containing transported clastics derived from nearby
granite- and schist exposures. Locally, sediments of Trubi-type, considered
by all colleagues to be an open marine deposit, seem to alternate with
Arenazzolo-like deposits. Ogniben (1957) described a gypsum-Trubi-Arenazzolo
succession, in turn overlain by Trubi from an area near Contrada
Drezzaria. In the area of Bosca-Stincone (Serradifalco, Caltanisetta) 10 to
20 m of Arenazzolo are intercalated in the Trubi some tens of meters above
its base. Similar successions seem to occur near Mimiani (Caltanisetta) and

Mappa. These successions are hard to explain if one considers the Arenazzolo
to be of lacustrine origin, and even more enigmatic if one considers the Trubi
to be an abyssal deposit.
The Arenazzolo as a sediment, together with its faunal content, makes
sense in a shallow or marginal marine environment in which more normal
and open marine conditions were gradually introduced, either as a result of
slow basin floor subsidence or of a gradual rise in sea level. The supply of
fine terrigenous clastic material decreased to between 30 and 40% and
biogenic sedimentation started in the off-shore area.
In our opinion Ogniben (1957) was correct to regard the Arenazzolo as a
transgressive sequence. It is transgressive at least in the sense that salinities
were closer to normal than during the preceding evaporation phase. Drooger's
opinion (1975) that it is of regressive character is based entirely on the
assumption that undisturbed growth of selenitic gypsum at Capo Rossello
took place at greater depth below wave base than the deposition of the crossstratified
sands. Possibly the Arenazzolo sedimentation took place at rapidly
varying depths, even allowing fresh-water lake deposits with Cyprideis to
become intercalated, but the overall tendency is transgressive. It would be
better to consider the Arenazzolo as an initial phase of the Pliocene Trubi
sedimentation than as the terminal phase of the evaporation cycles of the
Messinian.

LITHOLOGY
The new exposure to be dealt with is along the beach of Eraclea Minoa.
The outcrop is numbered 3, to avoid confusion with the two earlier described
and numbered sections from the same locality (Brolsma, 197 5b). An
accurate description of the section's attainability is given by Brolsma (197 Sa,
p.97).
Section 3 is situated only 300 m SW of section 2 (fig. 2), and was brought
to the attention of the author by Dr. N. Ciaranfi (Bari) during the excursion
organized by the Erice seminar, in 1975. The general change in lithology in
the transitional interval between Arenazzolo and Trubi, has been described
and discussed before (fig. 5; op cit. 1975b). In exposure 3 an entirely new
type of succession is formed by an intercalation of Trubi-like limestones
within this transitional interval. This thin interbed of only 7 to 8 cm in
thickness shows a gradual lower contact with the underlying black coloured
clays, whereas its upper boundary is sharp and straight with a sandy layer of
equal thickness on top. Upwards, this fine-grained, well sorted sand bed
rapidly changes into burrowed, blue coloured clayey marl which turns into
harder, more cream coloured marl and finally into indurated, compact Trubi
limestone. This entire sequence has a thickness of only 40 cm (fig. 6).
The thin intercalation of Trubi limestone in this transitional sequence
again indicates that the change in facies from Arenazzolo to Trubi was a
gradual process which progressed by fits and starts. The return of clastic
supply after a short period of biogenic sedimentation cannot be explained
in terms of great or sudden changes in water depth. It is more likely that
the supply of terrigenous clastic fines decreased, permitting biogenic sedimentation
in a progressively ingressing sea (Brolsma, 1975b, p. 377). Superimposed
on this gradual change in depositional environment, terrigenous
material was incidentally supplied, which resulted in the positively graded
sandy intercalation. Subsequently, Trubi sedimentation, which elsewhere
probably continued during this short episode, gradually became reestablished.
Similar sequences of events have been reconstructed and discussed before
on the basis of the data supplied by Ogniben (1957). However, the scale
at which various lithological types alternate in this section is much smaller.
It has been observed that near the basin margins the Trubi and Arenazzolo

Transitional interval showing the gradual lithological change from dark Arenazzolo clays
to cream-coloured, marly Trubi limestones at Eraclea Minoa (exposure 2).

may interfinger. Evidently biogenic sedimentation had already started while
at other places the Arenazzolo was still being deposited. Sedimentation of
the Trubi was locally interrupted by renewed supply and deposition of
coarser terrigenous material. Such alternations are normal features in marginal
areas displaying rapid horizontal changes in environmental conditions,
which may become reflected in vertical sections. Such rapid variations in
depositional types may be expected to become strongly reduced to scale,
or to be absent, in the more remote, i.e. central parts of the basin, such as
in the successions along the sourthern coast of Sicily.
The wash residues of the four samples collected from the newly described
transitional interval at Eraclea Minoa clearly reflect the different lithologies.
The Trubi intercalation contains the smallest number of mica flakes. The
underlying and overlying samples contain large amounts of mica, gypsum
and pyritic grains in addition to other clastic debris. The topmost sample
of this transitional interval again contains less mica.
The conservation of the foraminiferal tests is good in the Trubi intercalation
and transitional marls (sample 4). Brown ferruginous coatings are
frequent on the benthonic tests in the other two samples. The planktonic
foraminifera in the latter two samples are much better preserved than the
benthonic foraminifera.
Only 20 benthonic species have been recorded in a total of 100 counted
specimens in the Trubi intercalation (fig. 6), whereas 42 to 47 species were
encountered in the other three samples. The Trubi intercalation (sample 2)
is 4gminated by five benthonic species; in descending order of abundance
these are: Gyroidina soldanii, Dentalina filiformis, Epistominella exigua,
Oridorsalis umbonatus and Gyroidina umbonata. All five species are frE'quent
elements in the overlying Trubi sediments (cf. Brolsma, 1975b, figs. 7 and
13). In the other three samples Ammonia beccarii, Bolivina species, Bulimina
species, Elphidium species and epiphytes are the most conspicuous
elements. The number of benthonic specimens per 200 counted planktonic
specimens is 10 and 15 in samples 1 and 3, but less than 1 in samples 2 and
4. Smaller quantities of planktonic forms in samples 1 and 3 are held responsible
for the relatively high number of benthonics per 200 counted
planktonic individuals. In samples 2 and 4 planktonic foraminifera are very
abundant and no benthonics were encountered in the total of 200 counted
planktonic specimens. The occasional presence of Globorotalia margaritae
(primi tiva-type) in samples 1 and 4 is worth mentioning.

2 3 4
2 3
1 5
2 6
1 8
10
1
1 9
2 4
1 4
5
1
4
4
3
4
2
6
4
7
3
4
1
1
3
3
1
6
5
3
1
6
4
2
2
4
1
3
16
1
45
100
~
Ammonia beccarii
Bolivina antiqua
Bolivina dilatata
Bolivina plicatella var. mera
Bolivina reticulata
Bolivina spp.
Bulimina aculeata
Bulimina spp.
Cassidulina laevigata
Cibicides pseudoungerianus
Cibicides refulgens
Cibicides tenellus
Dentalina filiformis
Elphidium spp.
Epistominella exigua
Fissurina spp./Lagena spp.
Gyroidina orbicularis /parva
Gyroidina soldanii
Gyroidina umbonata
Hanzawaia boueana
Melonis barleeanus
Oridorsalis umbonatus
Rosalina globularis
Stilostomella adolphina
Globocassidulina subglobosa
Astrononion italicum
Cassidulina laevigata var. carinata
Cibicides bradyi
Nuttallides rugosus var. convexus
Cibicides lobatulus
Miscellaneous
Indeterminable
Total number of counted species
Total number of counted specimens
Number of benthonics/200 planktonics
Lithostratigraphic column of exposure 3 at Eraclea Minoa with the distribution of the
benthonic species.

CONCLUSIONS
The mediocre preservation of the benthonic fauna in samples 1 and 3,
combined with the high diversity may be due to mixing of faunas from
different habitats. Epiphytes, Elphidium and A. beccarii are normally not
found living in association with so many mud-preferring forms of the genera
Bolivina and Bulimina (see also Brolsma, 197 5b). The superior preservation
of the planktonic foraminifera in these two samples may indicate their
autochthony. Evidently such faunal mixing did not take place during the
deposition of the Trubi intercalation as is shown by the excellent preservation
of the tests and the conspicuous drop in species diversity. In the topmost
sample, only the epiphytes (Cibicides refulgens, Cibicides lobatulus
and Rosalina globularis) and A. beccarii may show a brown colouring whereas
all other faunal constituents are beautifully preserved. It appears as if only
the brown coloured specimens are allochthonous and may have been carried
to the area of deposition either in suspension together with the clay fraction
or as elements clinging to drifting submarine vegetation.
The Trubi intercalation clearly represents an altogether different facies
in which fewer and different taxa rapidly occupied the newly introduced
ecological niches. The incidental supply of terrigenous material carrying
the marginal faunas disturbs this sequential pattern, resulting in the sudden
increase in diversity of benthonics and an increase in B/P ratio. As soon as
the coarser material had settled the autochthonous assemblage returned.
Obviously the introduction of the foreign elements was a rapid process
prohibiting a thorough mixing of indigenous and allochthonous assemblages.
Taking into account only those forms that constitute 5% or more of
the assemblage, the minimum depth of deposition of this Trubi intercalation
would be 40 m, based on the deepest recorded upper depth limit,
that of Gyroidina soldanii (Drooger and Kaasschieter, 1958). The maximum
depth of deposition is represented by the shallowest lower depth limit of
one of the five dominant species, which is Dentalina filiformis at 2400 m
(Blanc-Vernet, 1969). The most likely depth of deposition is formed by
the preferential depth occurrences of all dominant forms combined, which
in this case very vaguely centres around 100 m (cf. figs. 25-26). A depth of
deposition between 50 and 200 m has been considered likely for the Arenazzolo-Trubi
transitional interval at the other localities of Eraclea Minoa and
Capo Rossello (cf. Brolsma, 197 5b). So it seems as if the benthonic Trubi
fauna of sample 2 does not indicate a greater depth of deposition but rather
a different environmental realm in which accumulation of skeletal debris
of nannoplankton and foraminifera prevailed, incidentally disturbed by
influxes of terrigenous detritus carrying displaced, marginal faunas in suspension.

A composite section of the Trubi is exposed along the beach of Capo
Rossello and in the cliffs around Lido Rossello (fig. 1). Its lower and upper
contacts are well exposed. Numerous normal faults trending NW-SE divide
the Trubi into separate compartments, on the average some 50 m wide.
The throw along these fractures seems to be small, not exceeding 10 to
15 m. Within each compartment reliable profiles can be sampled. Correlation
between one block and the other is often more difficult. For our study we
primarily sampled in detail the lower 40 m, exposed in an easily accessible
gully which ends at the beach (section 3, fig. 1) some 250 m NW of the
Miocene-pliocene boundary stratotype locality (section 2, fig. 1). In a
vertical sense the section is continuously exposed. The dip of the strata within
this tectonic block is negligible. Eight meters in the upper part of the section
was sampled in still greater detail for the "Accuracy in time" project
(Utrecht Micropal. Bull. 17). The upper 10 m of the Trubi were sampled at
two localities: Lido Rossello (section 5, fig. 1), and Punta Piccola, some 4
kilometers east of Lido Rossello (fig. 1). At both localities the marls of the
Monte Narbone formation follow in an upward direction. The Trubi sediments
in Capo Rossello, situated between the lower 40 m and the top, were
not sampled in comparable detail, for the tectonic reasons outlined above
(section 4, fig. 1). Sections 1 and 2 have been the subject of earlier publications
(Brolsma, 1975b).
The Trubi has a thickness of 100 to 120 m at Lido Rossello (Cita, 197 Sa,
fig. 10). It either starts from a disturbed contact at its base (section 2,
fig. 1, Miocene-pliocene boundary stratotype) or it has a transitional interval
(section 1) straddling the boundary with the underlying clastic Arenazzolo
(Brolsma, 1975b). The transitional interval shows plastic blue clay below,
which rapidly becomes marlier ,harder and more cream coloured in an upward
direction, and which in turn passes into the true biogenic limestones
of the Trubi type (fig. 7). Burrows filled with contrasting blue and cream
coloured sediment are present in this transitional interval but burrowing
is not held responsible for the gradual change in lithology.

107
107G
B.C
107A
106
1394
64
1393
EJ::IJ Marly
limestone
EtJ3 Clayey limestone
I~~IMarl
t..--...-j Marly
cloy
--------------. Undulating lithological boundary
___ Sharp lithological boundary
- - - - Gradual lithological change
;J Bioturbation
V0
Load casts
~ Undulating lamination
---L.- Oblique lamination
p
Increasing
Pyrite
pi Plant remains
ex
Fish remains
induration
Pyritic levels or nodules
in situ or displaced
® Mollusc remains
Ferro - mangonese- rich
i nterVQ I s
Gypsum
crystals
Lithostratigraphic column of exposure 3 at Capo Rossello showing the position of the
samples. The legend is valid for figure 39 as well.

Section 3
The sampled section 3 covers an interval of some 47 m. The lowermost 6
to 7 m of the generally cream coloured Trubi are characterized by vaguely
bedded, intensely burrowed (fig. 7), compact limestones (samples 1393-
1397, fig. 8). The bedding is mainly caused by clayey-marley horizons of
irregular lateral extension, which are 10 to 15 cm thick. On larger surfaces
in the ()utcrops the compact limestones show spheroidal weathering.
Upwards, the lithology changes into a rapid alternation of relatively soft
and marly, and more indurated limestone beds (samples 65-70, 1399-
1400). The greyish marly limestones grade upwards into the compact limestones
which show brown, indurated and apparently more strongly burrowed
surfaces at their top. The marls may contain dark brown to green clay
seams. The thickness of such small sequences varies from 30 to 70 cm; on
a total thickness of 10 meters, 25 of such sequences may be distinguished.
The next 10 m comprise limestones with a thickness of 1 to 1.20 m,
separated by more marly beds of only 20 to 40 cm (samples 71-1404). The
well-bedded appearance of the underlying part of the Trubi tends to vanish,
the marly levels becoming more compact.
The following 1.6 m consist of more marly limestsmes (35 to 60 cm)
which alternate with harder limestones of some 20 cm (sample 1405).
Upwards, a limestone bed with a thickness of about one meter, is characterized
by several thin, subhorizontallevels consisting of relatively indurated
material, showing a black interior. Oblique, U-shaped burrows filled with
similar resistant material are abundant; the black core is supposed to be
pyrite; the outer coating contains a mixture of gypsum, calcite and jarosite
(cf. Brolsma, 197 5b).
The next higher 8 meters are characterized by the presence of six levels
of brownish-rose, finely bedded to laminated limestone which are intercalated
in a succession of both marly and indurated limestones (samples
73-101). This part of the Rossello 3 section was sampled again (CRP 8-45)
for the analysis of counting methods. The alternative description of these
8 meters are published in Utrecht Micropal. Bull. 17 as well, together with
the results of the micropaleontological investigation.
The lowermost 40 cm of this 8 meters interval show indurated pyritic
. levels at the base and finely laminated, rose coloured sediment on top.
Within this bed, semiglobular, asymmetrical bodies of homogeneous limestone
are embedded in the laminated deposits (fig. 9). Burrows are numerous
and some of them are composed of the same brown-black material as described
above. Sample 73 was collected from a semiglobular body. Within the

Fig. 9 Laterally displaced loadcast-structures at the base of the laminated/non-laminated interval
of the Trubi at Capo Rossello, exposure 3. Note the fine-bedded character in the upper
part of this figure.
upper 6 cm of this bed, a rose coloured, finely bedded stratum with a thickness
of 2 to 3 cm is intercalated.
The lowermost laminated to finely bedded interval of substantial thickness
(about 140 cm, fig. 9) shows a gradual transition over a few centimeters
from the underlying deposits, due to an irregular alternation of non-laminated
(sample 74) and finely laminated, brownish beds. In an upward sense,
the limestone beds decrease in thickness from 2 cm to less than 0.5 cm over
an interval of 10 cm. The fine lamination is traceable due to differences in
induration of the laminae, probably caused by different iron-contents.
Burrowing has not disturbed the lamination; however, the upper part of this
unit is distinctly burrowed, without substantial distortion of the lamination.
Here, the lamination is more delicate and wavy in a somewhat more brownish
sediment. The burrows have a length of up to 10 cm; they are oblique to
subparallel with respect to the original lamination (fig. 10) and filled with
contrasting greyish material derived from the overlying marly limestone.
Samples 75 to 78 were collected in this first laminated interval.
The basal part of the overlying grey marly limestone is burrowed as well,
causing a gradual transition (sample 79). These burrows are filled with rose

sediment, corresponding in colour to that of the underlying bed. The basal
marly limestone (sample 80) passes upwards into brownish and indurated
limestone (sample 81). The total thickness of this unit amounts to 50 cm.
The lower boundary of the second finely laminated unit is marked by
a rapid change in colour to rose-brown. The sediment seems to be clayey;
burrowing is present but rare. Some less distinctly laminated interbeds have
a thickness of up to 4 cm. Samples 82 and 83 were collected in this 60 cm
part of the succession. At the top of the previous unit the sediment changes
into a light brown, less distinctly bedded limestone, which contains burrows
filled with white limestone of pelletoidal texture. This sediment passes in
turn into homogeneous limestone which is overlain by a laminated bed with
a thickness of 6 cm and a compact, indurated limestone of 15 cm (sample
84). The unit ends with a marly, partly laminated limestone of 20 cm thickness
(sample 85).
The undulating lower contact of the third laminated unit of rose-coloured
sediment (thickness 45 cm) is rather sharp and well traceable in the horizontal
sense. The sediment is of remarkably low weight and shows delicate
lamination with small scale undulations, draping over larger specimens of
Fig. 10 Horizontal burrows on a bedding plane in a laminated interval of the Trubi at Capo Rossello
(exposure 3).

Orbulina, which in turn seem to depress the laminae underneath. Fish remams
are common.
The variation of hues from white to brown shows that the lamination
is discontinuous in a lateral sense. Inclusions of greenish clay may be caused
by burrowing but since the lamination seems to follow the outlines of the
inclusions at least part of them may be pebbles (diameter up to 2 em).
The lamination shows internal unconformities as well as wavy stretches
with a height of 0.5 em. The lower contact of this unit is irregular due to
folded structures and the occurrence of oblique lamination, visible over a
horizontal distance of up to 20 em. The folded structures have a width of
some 10 em. Internal small scale, zig-zag folding of laminae has been observed
as well. Samples 86 and 87 were recovered from the base and top of this
unit, respectively.
The third laminated unit is covered by 20 em of marly limestone with a
distinct lower contact and intense internal bioturbation. Sample 88 was collected
from this level.
The fourth laminated bed has a thickness of only 25 em. Upwards, it
changes gradually but rapidly into a burrowed limestone. Near its base,
sample 89 was collected.
On top we find a compact, burrowed limestone of 20 cm (sample 90),
followed by a relatively clayey limestone of brown colour (10 em, sample
91) which gradually passes into an indurated limestone of 30 cm (sample
92). The pronounced top of this limestone is covered by 30 em of marly
limestone (sample 93), which upwards shows an increase in clay-content and
a change to brownish hues (20 cm). The total thickness of this non-laminated
unit is 110 cm.
At the level of sample 90, the investigated section had to be shifted 2.5 m
to the SSE, for reasons of accessibility.
Upwards, the fifth laminated intercalation attains a thickness of 60 em.
Burrowing is present without destroying the delicate bedding; the thin beds
are homogeneous and white. In the lower part sample 94 was collected.
About halfway, a relatively indurated, thin bedded intercalation is observed.
Towards the top, burrowing and clay content increase; here, lamination is
restricted to some levels, while the sediment-colour changes to brown. In
one horizon plant-remains are common. Sample 95 is located in this upper
clayey part.
The clayey top part of the fifth laminated intercalation gradually changes
into a marly limestone of grey colour (sample 96). This grades upwards into
somewhat more indurated limestone (sample 97). On top we find marls
and marly limestone, showing an upward increase of induration (samples

98 and 99). The total thickness of this unit is 150 cm.
At the top of this 8 meters interval there is a sixth unit with laminated
sediments of some 50 cm thickness. The internal bedding is disturbed by
burrowing in its lower and upper parts. About half way, less intensive
organic activity allowed the preservation of discontinuous laminae. Sample
100 was collected from this middle part. In upward sense the sediment
changes rapidly into a relatively indurated, brown coloured and burrowed
limestone (sample 101).
Two meters of soft and marly limestones with intercalations of more
compact beds follow on top (samples 102-104). Higher up the marly
intercalations disappear, and the vaguely bedded and massive character
found in the basal few meters returns (thickness 6 to 7 m, samples 105-
107). At the boundary between two of the compact limestone beds, a
very thin clay seam was observed, which pinches out laterally to continue
as a red-brown coloured bedding plane. It could not be verified whether
similar bedding planes correspond to comparable clay seams in a horizontal
direction.
Some two meters below the top of the section a 50 cm clayey intercalation
is of special interest. The base of the clay is irregular. In a lateral sense
it shows a horizontal offshoot of 2 cm (sample 107 B) to zero under a wedge
of the underlying limestone and over a lateral distance of some 30 cm (fig.
11). The clay body is of dark green colour (samples 107 D-F). Larger, brown
coloured burrows (diameter 1 cm) usually follow horizontal paths. Smaller,
white coloured and bifurcating burrows form a system of branching tunnels
(fig. 12 and 13). Oriented samples show these tunnels to branch in a downward
direction. The tunnels are circular in cross-section and have a constant
diameter of about 1 mm. At some levels discontinuous lamination is still
preserved. The over- and underlying indurated limestones show no bioturbation,
but the contact between the clay and the overlying limestone is
burrowed (sample 107 G).
The top of section 3 shows gravels and soil in unconformable position.
Near Lido Rossello, to the west, the Trubi attains a greater thickness, of
more than 100 m. It passes upwards into marly sediments with intercalations
of brownish colour, which are unconformably covered by Quaternary
calcarenitic sands.
62 samples have been taken from section 3. The sampling was focussed
on the indurated/non-indurated sequences (20 samples) and the alternation
of laminated/non-laminated sediments (29 samples).

0 10 20cm.
L--L--J
~II\\
:::0 if.- :::0 :::"
OJI
OJI
II
II
II
ABeD E F G
107A 107B 107C 107D 107E 107F 107G
1 2 1 2 1 3 2 Astrononion italicum
1 1 1 1 1 Bolivina spp.
4 5 4 1 10 2 4 Cibicides bradyi
3 3 2 Cibicides italicus
1 2 2 4 Cibicides pseudoungerianus
1 1 2 1 Cibicides spp.
1 5 1 3 1 2 5 Eggerella bradyi
1 2 2 1 2 Flori/us grateloupi
3 1 1 4 2 4 4 Gyroidina umbonata/orbicularis
5 1 5 1 3 2 4 Oridorsalis stellatus
1 5 2 3 2 1 Oridorsalis umbonatus
10 5 4 9 5 2 3 Pullenia spp.
14 4 11 8 11 9 Siphonina bradyana
4 3 1 1 Dentalina spp.
3 4 4 1 Fissurina spp./Lagena spp.
2 6 2 Hanzawaia boueana
1 2 3 Lenticulina spp.
1 2 1 3 Oolina hexagona
3 Nuttallides rugosus var. convexus
4 2 Pleurostomella spp.
2 9 7 7 5 9 5 Miscellaneous
16 28 22 26 23 22 19 Total number of species
1 1 1 5 3 3 Total number of benthonics/200 counted planktonics
1 1 1 2 1 Indeterminable
50 50 50 50 50 50 50 Total number of counted specimens
Fig. 11 Lithostratigraphic column of a clayey interval of the Trubi in the top part of exposure 3
at Capo Rossello with the distribution of the benthonic species.
Section 4
Forty meters of Trubi limestone which are considered to overlie the strata
of section 3 have been sampled (17 samples) in section 4 (fig. 1). Strong
deformation of the topmost laminated interval at this locality shows that
displacement has taken place after deposition of the sediment. Only four of
the samples were studied from this middle part of the Trubi to check

Figs. 12 and 13. Chondrites-burrows in the topmost clayey interval of the Trubi at Capo Rossello
(exposure 3).

whether its assumed intermediate stratigraphic position was substantiated by
the planktonic markers (samples 42-45, some 30 m stratigraphically above
107). The benthonic fauna was studied for comparison with the overlying
an'd underlying assemblages. This middle part of the Trubi is well-bedded.
Minor lithological differences between the consecutive beds are shown by
selective weathering, but in fresh outcrops these differences are hardly
detectable. Horizontal partings may contain thin clay seams which show
discontinuous lamination and mottled structures. Small, bifurcating burrows
as described from section 3 were found in this middle part as well.
Section Punta Piccola
The uppermost part of the Trubi, exposed in the Punta Piccola section,
is very similar to the lowermost few meters at Capo Rossello: thick bedded,
highly indurated and thoroughly burrowed (samples PP 1-7, some 60 m
stratigraphically above 107). Burrowing is visible by brown and blue coloured
stains with diameters of 1 to 2 cm. The burrows seem to diminish in
diameter in an upward direction because the brown coloured spots are
smaller with diameters of 0.5 to 1 cm; they may be surrounded by concentric
rings of 1 to 3 cm diameter.
Discussion of the lithology
In general, Trubi sediments consist for some 75% of carbonate of mainly
planktonic origin, for some 25% of silica and clay minerals. Low sedimentation
rates and favourable conditions for bottom life may explain the vague
bedding, intense burrowing and compact character of the lowermost 6 to
7 m of the limestones. Burrowing activity evidently destroyed any stratification
that might have been present. Sedimentation rates may have increased
occasionally to account for the few more clayey intercalations.
The distinct bedding higher in the section is caused by marly intercalations
possibly indicating periodical supply of fines. The dark coloured clay
seams within the marly intercalations indicate homogenization to have been
less at times; the decreased burrowing must be due either to increased sedimentation
rates or to less favourable bottom conditions. The observed
25 gradual changes from marl to indurated limestone may either be explained
by decreasing supply of terrigenous fines or by an increasing activity of
burrowers enhanced by either a decreasing rate of deposition or by improving
bottom conditions. A varying rate of deposition caused by a fluctuating
supply of terrigenous fines seems to be the most plausible mechanism
for the rhythmic type of sedimentation. Indications for a turbiditic type of

sedimentation have not been found. The hardground-like character at the
top of the indurated limestone part of the cycles was not found to be
correlated with any notable change in benthonic fauna that might indicate
sudden changes in bottom conditions.
Upwards, the supply of clay seems to decrease, allowing burrowers to
homogenize the sediment again in 1 to 1.2 m thick beds. More marly intercalations
of only 20 to 40 cm indicate that the supply of fines had not
ceased completely. Before the onset of a different type of sedimentation
the supply of terrigenous fines briefly increased over an interval of only
1.6 m.
The various brown coloured, pyrite containing subhorizontal levels
within the thick limestone bed at the base of the laminated/non-laminated
part of the section may have been formed as a result of negative Eh conditions
below the sediment-water interface, caused for instance by high quantities
of decomposing organic detritus (cf. Brolsma, 1975b, p. 362). Similar
material fills the U-shaped burrows in which comparable reactions have
probably played a role. Finely bedded sediments appear to be associated
with similar pyritic inclusions in the overlying bed. Burrowing organisms
evidently did not destroy this fine bedding. High organic productivity in
the overlying water column may have enhanced the subsurface formation
of pyrite and obstructed the activity of burrowers. Oxygen depletion below
the sediment-water interface may at times have extended up to this interface,
resulting in still further deteriorating bottom conditions.
The sack-like structures in the overlying bed are interpreted as the result
of loadcasting. The slight lateral component probably was caused by gliding
movements toward the south east, as is concluded from the orientation of
the axial planes of the loadcasts. These features indicate rapid deposition as
well as a dip of the seafloor toward the south east. This possibly indicates
that the deeper part of the basin was located SE of Capo Rossello.
The gradual transition at the base of the first laminated interval of substantial
thickness may be best explained by an alternation of periods of
higher productivity increasing the rate of sedimentation, and periods of
lower productivity and consequently lower sedimentation rates. The intensity
of bottom life varied accordingly but never ceased completely. Even the
finest laminated parts show small burrows which do not disturb the lamination.
Such laminated or finely bedded sediments may even be present in the
more indurated, seemingly homogeneous limestones as thin intercalations,
which indicates the fluctuating character of the poor bottom conditions in
the course of time.
Occasional oblique or subhorizontal burrows of greater dimensions indi-

cate that larger burrowing organisms survived during such periods of high
productivity and increased sedimentation rates.
The wavy stretches and folding structures of the laminae, especially at the
base of the third laminated unit may point to instability of the unconsolidated
sediment on a dipping seafloor shortly after deposition; internal
cohesion in the sediment was sufficient to allow the formation of small
zig-zag folds.
Burrowing activity during sedimentation of the intercalated marls and
limestones frequently blurs the boundaries with the laminated units. The
amount of clay admixture seems to vary and is for instance higher in the
second and fifth laminated units. Also the numbers of radiolarians and
diatoms in the wash-residues vary from abundant to negligible from sample
to sample within a single unit. The light-weight sediment of the third laminated
unit contains relatively large numbers of diatoms and radiolarians.
Laminae are found to drape over relatively large specimens of Orbulina
and pebble-like inclusions, whereas these larger objects in turn are seen
to depress the underlying, unconsolidated sediments.
The presence of plant remains at one level in the fifth laminated interval
points to an ample supply of allochthonous material. The morphology of
these remains is similar to that of Posidonia weeds, which suggests that the
plant material drifted in from shoaler areas.
The sixth and uppermost laminated interval forms the end of this period
of variable sedimentation rates and corresponding periods of faunal and
floral blooms. Only in the middle part of this uppermost laminated interval
was burrowing activity unable to destroy the fine bedding.
After the deposition of the sixth laminated unit the overlying marls and
limestones suggest environmental conditions similar to those below the
silica-rich and finely bedded part of the section. Biogenic sedimentation
with slow deposition rate and favourable bottom conditions allowed burrowers
to homogenize the sediment, as in the basal part of the section.
Depositional rates may have increased occasionally to account for the thin
clay seams separating the compact limestone beds.
Increased clay supply may account for the homogeneous as well as the
discontinuously laminated levels within the 50 cm clay layer at the top of
section 3. The bifurcating burrows observed in these clays are considered to
have been caused by the ichnogenus Chondrites Sternberg (1833). Good
descriptions of such fossils have been given by Simpson (1957) and by
Hantzschel (1975). According to Simpson the maximum ratio of tunnel
length to tunnel diameter is 40, which would mean our specimens were 4 cm
long. Actually, this is the maximum length measured in our material. Chon-

drites are trace-fossils consisting of a system of regularly branching tunnels
of uniform diameter, formed by some animal working from a fixed basepoint
at or just below the seafloor. It is a cosmopolitan genus, reported with
certainty from the Ordovicium to the Tertiary. Our Trubi specimens show a
layered, carbonate filling which is more indurated and of lighter colour than
the surrounding sediment. Preferential induration of such tunnel fillings has
been noted before by Kennedy (1970). The entire genus Chondrites undoubtedly
belongs to the Fodichnia and has to be regarded as feeding structures
of sediment-eating animals and not as dwelling burrows of filter-feeding
annelids (Seilacher, 1964). Simpson regards these burrows as the result of
sipunculoid (= unsegmented) worms working from a fixed centre at the
surface of the sediment and producing tunnels by an extensile proboscis; the
branching pattern may be caused by phobotaxis (= behaviour to avoid
penetrating its own tunnel or the tunnel of others in its passage through the
sediment).
A bed with Chondrites is of marine origin and the water was not greatly
agitated by wave-action (Simpson, 1957, p. 494). Warme et al. (1973) stated
that Chondrites has little value as a bathymetric indicator, being cosmopolitan
and crossing both bathymetric and lithologic facies boundaries. But
the presence of this trace fossil requires that the bottom waters be oxygenated
when the traces were formed, and that the sediments contain sufficient
food.
The middle part of the Trubi in section 4 with its well-bedded appearance
resembles the lower part of the Trubi on top of the basal 6 to 7 m of vaguely
bedded, compact limestones. A variable rate of deposition caused by a
fluctuating supply of terrigenous fines seems to be valid for this part of the
section as well. The presence of clay-seams in horizontal partings and the
presence of Chondrites point to sedimentation conditions comparable to
those described for the lower part of the section.
A low rate of sedimentation enabling burrowers to homogenize the
sediment returns in the topmost Trubi part at Punta Piccola. Bottom conditions
apparently remained favourable for bottom-dwelling life. Pyritisation
in boreholes seems to be responsible for the concentric rings around the
observed pipes. The upward decrease in diameter of the burrows may point
to an unknown change in biotope favouring smaller sized burrowers.

The foraminiferal faunas from the Trubi, of which 73 samples have been
studied, are characterized by good preservation and normal sized tests.
Broken specimens are scarce, with the exception of those in sample 1400;
only a small number of specimens is indeterminable. A few tests may be
coated with either limonite, pyrite or carbonate thus obscuring characteristic
features. Most Oolina hexagona specimens in sample 77, forming 97% of the
fauna, show both carbonate and black coating.
In the lower part of the Trubi (samples 1393-1405) an admixture of
badly preserved benthonic specimens was observed. These forms are either
etched, worn or vitreous and of light brown colour. They belong in particular
to planoconvex representatives of Cibicides, especially of refulgens type,
Anomalina helicina, Elphidium, Uvigerina, Bolivina and Quinqueloculina
species, and sometimes Pullenia. The admixture of such badly preserved
forms becomes strongly reduced or absent in the overlying part of the section.
The benthonic fauna of sample 1395 is almost entirely composed of
such badly preserved forms except for a few representatives of Dentalina filiformis,
Globocassidulina subglobosa, Gyroidina umbonata, Oridorsalis umbonatus
and o. stellatus. It is this group that is constantly well preserved in
all samples from this lower part of the section.
B/P ratio
The number of benthonic individuals per 200 planktonic specimens varies
between 0 and 22 (fig. 14). Minimum values show an irregular pattern
throughout the Trubi column at Capo Rossello; they are common in the
laminated sediments. Marly-clayey samples below the second, third, fourth
and fifth laminated units appear to contain most benthonic forms and show
a steady increase from 11 to 22 per 200 planktonic individuals (samples
80, 85, 88 and 93). Between the fifth and sixth interval and on top of this
uppermost laminated bed, benthonic forms are relatively scarce again and
the actual numbers show minor fluctuations only. No relation is observed
with the different types of sediment in the hard-soft sequences (samples
65-70). The four samples from the middle part of the Trubi in section 4
contain benthonic faunas in quantities comparable with those of the lower
part of the Trubi (figs. 14 and 15). The number of benthonic specimens has

45
42
\ Sample numbers
I'
'07
107G ~-
~ >8
"
107 A
'd.
102
6 100
97
5
92
4
87
84
82
80
7.
73
1405
1402
72
7'
1400
1399
70
.7
.5
1397
1394
.4
1393
Graph showing the numbers of planktonic (A) and benthonic (B) species in the consecutive
countings as well as the Fisher a-diversity indices (C) for the benthonic faunas from the
lower and middle parts of the Trubi at Capo Rossello (exposures 3 and 4). In the right
hand column the number of benthonic specimens per 200 counted planktonic individuals
is reproduced (D).

42 43 44 45 sa~
3 4 4 Astrononion italicum
3 6 6 2 Bigenerina nodosaria
1 2 2 2 Bolivina spp.
4 5 5 7 Cibicides bradyi
4 1 2 1 Cibicides lobatulus
2 3 2 1 Cibicides pseudoungerianus
4 3 4 1 Cibicides spp.
1 1 3 3 Den talina filiformis
2 3 2 2 Eggerella bradyi
1 4 3 1 Globocassidulina subglobosa
1 1 1 Gyroidina soldanii
1 3 3 Gyroidina umbonata
3 1 1 8 Hanzawaia boueana
3 5 2 Karreriella bradyi
6 1 2 5 Lagena spp./Fissurina spp.
2 2 3 3 Lenticulina spp.
6 3 3 Melonis barleeanus
1 2 4 4 Oridorsalis stellatus
1 2 2 Oridorsalis umbonatus
2 3 2 1 Pleurostomella alternans
13 11 12 14 Pullenia spp.
1 4 1 4 Arenaceous
24 13 17 6 Siphonina bradyana
1 3 1 1 Uvigerina proboscidea/ striatissima
2 3 7 Bolivina dilatata
3 1 Gyroidina orbicularis
1 6 5 Planulina ariminensis
3 Anomalinoides ornata
3 Dentalina communis
3 Pleurostomella rapa var. recens
2 7 3 7 Miscellaneous
7 1 4 2 Indeterminable
100 100 100 100 Total number of specimens
33 41 34 39 Total number of speci~s
16-18 25 16-18 20-25 Fisher a-index
0 1 4 4 Number of benthonic/200 planktonics
Fig. 15 Distribution chart of the benthonic species from the middle part of the Trubi in exposure
4 at Capo Rossello.
increased again (up to 9) in the top ten meters of the Trubi at Punta Piccola
(fig. 38).
The rough estimates of the number of benthonic specimens per 200 planktonic
individuals do not allow any interpretation of the minor fluctuations.
However, the peaks in samples 80, 85, 88 and 93 seem to be more reliable
(fig. 14). Either the abundance of benthonic forms increased or the number

of planktonic individuals decreased, or both. The abundance of planktonic
individuals per unit weight of sediment has been estimated by Zachariasse
(1978), who concluded that only the most outspoken maximum and minimum
values in the production of planktonic foraminifera, diatoms and
radiolarians occured simultaneously. Smaller variations in production cannot
be correlated with each other or with the different lithology types.
The recorded variation in B/P ratios may therefore be related to variations
in production of planktonic foraminifera, e.g. higher production in the
laminated intervals with correspondingly low B/P ratios (samples 75, 78, 83,
86, 87, 89, 94 and 95, fig. 14) and lower production in between these
laminated intervals corresponding to high B/P ratios (samples 80, 85, 88 and
93, fig. 14). On the other hand, the highest B/P ratios are attained in the
most clayey intervals (samples 88 and 93), which suggests that bottom-life
improved as a consequence of increased supply and deposition of terrigenous
fines.
Details of the eight meter "Accuracy" section
The incorporation of the 60 to 125 J1 fraction in our counts (cf. Brolsma,
1978) shows us that the benthonic faunas in the laminated units are less
poor than previously assumed. It appears that the fauna tended to become
dwarfed during these periods. The ecological stress at the bottom was
probably brought about by oxygen deficiency. Riedel and Sanfilippo (1978)
investigated the radiolarian assemblages from various levels throughout this
part of the section. The results of their quantitative study suggest that
several samples (CRP 22-29 and 36) from the third to fifth laminated interval
had been deposited under slightly cooler-water conditions than samples
CRP 14, 30, 31 and 37. Diatom and silicoflagellate assemblages studied by
Schrader and Gersonde (1978) from the same samples give similar indications.
The laminated units 3 to 5, documented by samples CRP 22,27,29,
29A, 36 and 37, are thought to represent intervals during which the primary
production in the surface water increased. The surface water temperature,
interpreted from the silicoflagellate assemblages, would be lower within
this group of units, and higher in the lower and upper part of this interval.
All these observations may be caused by strong upwelling and a rather
unstable stratification in the upper part of the water column due to turbulence.
This unstable upper water mass was probably separated from
a more stable water mass below.
According to Calvert (1966) there is sufficient silica available in normal
seawater, notwithstanding the low absolute concentration, to account for

the accumulation of silica-rich sediments, if there is a mechanism which
continuously supplies dissolved nutrients to the euphotic zone. Recourse to
volcanic sources for the silica is not necessary. An intermittent supply of
nutrients to the surface waters to enlarge the biomass production may just
as well have resulted from fluctuations in river-discharge.
Increased floral and faunal productivity in the upper water masses will
have caused increased biogenic sedimentation rates, which, inturn, will reduce
the number of bottom-dwellers in the counts to insignificance. Furthermore,
rapid deposition of great quantities of organic material might create
an oxygen deficiency at or below the sediment/water interface, thus further
obstructing bottom-life either at or below this interface. Oxygen depletion
of the bottom waters or topmost sediments will have followed only if the
water stratification remained unchanged. If a thermocline was present in
such a stratified watercolumn this would lead to the assumption of cooler
bottom water at Capo Rossello. This assumption receives support from the
presence, in appreciable numbers, of small specimens of Epistominella
exigua. This species prefers cooler waters, whether deep or shallow (Anderson,
1963; Anderson, 1975) and is reported in association with diatoms in
the Bering Sea (op. cit., 1963).
The sedimentary processes outlined above would explain the preservation
of the fine-bedding.
Species diversity
The Fisher ex-indexfor the benthonics is highly variable and shows fluctuations
between close to zero and 25 (fig. 14). The six laminated intervals all
show a distinct drop in diversity, more pronounced in some intervals than in
others. The irregularly fluctuating pattern of ex-valuesfollows the numbers of
benthonic species per sample fairly well, but it does not seem to correspond
to the oscillation pattern of the numbers of specimens per 200 planktonic
individuals. The ex-index shows higher values in the clays of samples 107
B-F and lower values in the under- and overlying, indurated limestone beds
(samples 107 A and G, fig. 11). Similar highly diverse assemblages appear in
the middle and upper parts of the Trubi in section 3 and at Punta Piccola.
Sample PP 3 even reaches a maximum of 32-33. The simple diversity
values shown in fig. 18, based on the total fraction counts, show an indistinct
increase across the entire interval with laminated sediments.
The considerable fluctuations in ex-valuesare not so clearly linked with
the lithological units. In the lower part of the section up to the first laminated
interval, the staggering increase may be the result of ameliorating or

stabilizing bottom conditions. The maximum diversity in samples 1393 and
1395 is probably caused by the addition of allochthonous faunal elements
to the indigenous fauna. The relatively greater, though variable proportion of
badly preserved specimens throughout this lower part of the section indicates
that the source of supply of reworked material had not yet been·
drowned. The source area probably receded rapidly, to vanish completely
after a relatively short duration of Trubi sedimentation.
Benthonic life evidently suffered during the periods of laminated deposition
and silica-enrichment, not only in number of species and in diversity
but also in size of the individuals. Within the upper parts of the second,
third and fifth laminated intervals the species diversity seems to increase
again, somehow anticipating the improved environments, while sedimentation
of laminated sediments still continued. These changes must pertain to
bottom-bound processes which are thought to have been influenced by
primary changes in the overlying water column. As soon as the supply of
nutrients in the surface waters falls off a gradual decrease of the organic
sedimentation rate will take place, resulting from the decreasing supply
of planktonic elements to the bottom. The lower rate of deposition will in
turn result in consumption of less oxygen at the bottom owing to the smaller
amount of decomposing organic material. Benthonic life will become
re-established and diversity will tend to increase before silica-enrichment
comes to a complete stop.
An opposite effect may explain the drops in diversity below the laminated
intervals 1 and 3. As soon as nutrients increase in the surface waters
the phytoplankton production will tend to increase, but it may take some
time before it leads to (near-)oxygen depletion at the bottom.
Silica enrichments shown by high quantities of diatoms and radiolarians
are not completely correlated with poor bottom conditions resulting in
laminated sediments. Some of the laminated intervals contain but few
siliceous organisms, whereas for instance in the homogenized limestone
intercalation between intervals 3 and 4 radiolarians and diatoms abound.
Apparently burrowing organisms were able to homogenize this thin interval,
indicating that bottom conditions were not too poor. If increased planktonic
life caused low oxygen contents of the bottom water, we may conclude that
blooms did not always effect non-calcareous, calcareous and siliceous planktonic
groups simultaneously in the same relative proportions. Inversely,
increase of planktonic life did not always lead to seriously deteriorating
bottom conditions.
The highly diverse communities that seem to have lived during deposition
of the upper part of the section at the level of samples 107 A-G appar-

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ently favoured clayey substrates but were incapable of pushing the B/P
ratios to notably higher values. The increased species diversity in the middle
(CR 42-45) but especially in the upper part of the Trubi (PP 1-7), indicate
favourable bottom environments. The latter seem to be brought about by
an increased supply of terrigenous fines, possibly a consequence of an
encroaching hinterland. The presence of small specimens of Chama in sample
PP 3 may support the latter hypothesis.
Distribution
of species
In the lower 6 to 7 m of vaguely bedded, compact limestones of section 3
Dentalina filiformis, Epistominella exigua, Globocassidulina subglobosa,
Gyroidina soldanii, G. umbonata, Oridorsalis stellatus, o. umbonatus and
Valvulineria glabra are, in various combinations, the most frequent faunal
constituents (samples 1393 to 1397). The frequency distribution of most of
the benthonic foraminifera throughout section 3 is shown in the chart of fig.
16. The chart of fig. 17 shows that dominance rapidly shifts from one species
combination to another. G. subglobosa, G. umbonata and o. stellatus
recur with high frequencies in the overlying assemblages, whereas notable
quantities of the others are more or less restricted to this lowermost interval.
Some of them played an important role already in the transitional interval
with the underlying Arenazzolo (Brolsma, 197 5b). The large numbers for
D. filiformis result in part from fairly numerous broken specimens, the
fragments of which have been counted as complete individuals. D. filiformis,
E. exigua, G. soldanii and o. umbonatus are dominant elements in the
lower part of the Trubi at Capo Rossello, as well as in the Trubi type intercalation
in the topmost Arenazzolo at Eraclea Minoa (cf. figs. 5 and 16).
Eggerella bradyi, Karreriella bradyi, Uvigerina peregrina, U. pygmea,
Cibicides bradyi and Oolina hexagona are additional common elements
with fluctuating relative weight in the overlying 10 m of alternating marly
and indurated limestones (samples 65 to 1400). The latter two species
continue to be present in equally high numbers in the following samples.
Florilus grateloupi, Hanzawaia boueana, Uvigerina peregrina and U. pygmea
form dominant faunal elements(> 5%) in this interval only. Siphonina
bradyana starts to increase in numbers in sample 1399. Globocassidulina
subglobosa disappears as a common element but returns in smaller proportions
in the middle and upper parts of section 3.
The following 10m of more thick bedded limestones show a strong increase
of S. bradyana and Pullenia species. Also Lagena and Fissurina as a group
become more numerous in this interval.

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Black dots indicate dominance in meagre assemblages.
199

The next higher part of the section with six laminated units shows impoverishment
of the faunas, especially in the laminated sediments. The
finely bedded and silica-enriched beds (samples 73-100) frequently contain
little more than O. hexagona in dominating quantities. In homogeneous
beds in this interval Nodosaria vertebralis var. albatrossi appears twice as a
very frequent faunal element (samples 79 and 88). Anomalina helicina,
Cibicides pseudoungerianus, Dentalina subsoluta, Nodosaria longiscata,
Planulina ariminensis, Siphotextularia concava and Uvigerina proboscidea
form additional elements which may be common in one or a few of the
samples from the limestone interbeds. Chama-remains have been encountered
in sample 94 (pers. comm. R. Daams).
A more detailed picture of the fauna in this part of section 3 is obtained
from the sample suite of the Accuracy project (Brolsma, 1978). These more
detailed distributional data are based on countings of the total size range
(including the 60-125 Il fraction), with a maximum of 100 counted specimens
per sample, even in the laminated interbeds. In fig. 18, the distribution
of the most conspicuous elements is reproduced graphically. On the
right hand side two columns have been added for the numbers of species
and the B/P ratios. The numbers of species appear to have increased because
the smaller sieve-fraction is included, especially in the case of the laminated
interbeds. O. hexagona is predominant in all these interbeds, especially in
the lower two. Fluctuations do occur within such interbeds if more than two
samples are available (e.g. samples CRP 8A-14). Nuttallides rugosus var.
convexus, Epistominella exigua, Bulimina elongata, Bolivina antiqua and
B. advena have not been recorded in the other countings due to their smaller
dimensions. Moreover, they are mostly absent or very rare in the 60-125 Il
fractions of the lower Trubi samples of which only the coarser fraction
(125-600 Il) was counted. These forms constitute a fair part of the assemblages.
As a consequence of the dominance of o. hexagona in the laminated
interbeds the numbers of most other species appear after calculation to be
negatively correlated with those of this species. Taxa that show positive
correlation with O. hexagona such as B. advena in the third, fifth and sixth
intervals are therefore more reliable for paleoecological conclusions.
The assemblages from the next higher part of the section (samples 101-
103) are comparable to those from immediately below and between the
laminated intervals. In the uppermost 4 samples (104-107), however, the
number of benthonic specimens is low once more.
The faunal composition in samples 107 A-G does not differ significantly
from that of the underlying and overlying levels 106 and 107 (fig. 11).

Siphonina bradyana and Pullenia are the most frequent elements. Cibicides
bradyi is abundant in sample 107 E and Hanzawaia boueana peaks in sample
107 D. In this latter sample small pelecypod (amongst which Chama) and
gastropod remains have been observed.
In samples CR 42-45 from the middle part of the Trubi in section 4, S.
bradyana and Pullenia species are again the most common faunal constituents
(fig. 15).
Fig. 18 Graphical representation of the vertical distribution of some selected taxa in the size fraction
larger than 63 }J., in an 8 meter thick interval of the Trubi (exposure 3) at Capo Rossel-
10. In the right hand column the number of species (A), and the number ofbenthonics (B)
per 200 counted planktonic individuals are shown. The latter values are based on countings
in the size fraction larger than 125}J..

Cibicides pseudoungerianus appears as a frequent element in the uppermost
part of the Trubi at Punta Piccola (PP 1-7), together with Planulina
ariminensis in somewhat smaller quantities (fig. 39). S. bradyana remains a
common species. The Fissurina/Lagena and Pullenia groups, Hanzawaia
boueana, Cibicides lobatulus and Uvigerina peregrina frequently occur in
appreciable numbers. In PP 3 small, juvenile, well-preserved Chama valves
have been recorded.
For section 3 the percentage distribution of all arenaceous forms combined
has been plotted in fig. 19 to check whether any vertical trend or correlation
exists with either the indurated/non-indurated limestone successions or
with the laminated/non-laminated sequences. High percentage peaks (19
and 24%) occur in the lower part of the Trubi (samples 66 and 72). No other
fluctuations appear to be systematic or significant. The percentages for the
laminated intervals are based on 50 or less specimens per sample; because
of the low reliability of the individual percentage values they have not been
included in the figure. The total percentage of arenaceous forms in all
samples from the laminated deposits combined (fig. 48) is slightly lower
(7.26%) than in the accompanying non-laminated sediments (9.23%).
The continuous presence of benthonic and planktonic foraminifera in
all samples from the Trubi, but especially in its lower part, is not in agreement
with the earlier observations on the same locality by Cita (1973).
According to Cita, the lowermost 210 cm at Capo Rossello (comparable
to, our samples 1393, 64 and 1394) above the unconformable Miocene-
Pliocene boundary are devoid of benthonic foraminifera, whereas samples
higher in the sequence contained only two or three benthonic taxa per
sample. Because our data are different Cita's environmental conclusions
based on the absence of benthonic life at the base of the Trubi limestone
cannot be supported. The suggested great depth of deposition of the Trubi
limestone, in excess of 1000 m, probably of some thousands of meters,
based on the scarcity of taxa per sample is due for reconsideration.
In the lower part of the Trubi muddy-substrate preferring elements successively
replaced the typical Bolivina/Bulimina associations of the Arenazzolo
and the transitional clays and marls. Apparently the newly introduced
mud-feeders were more successful in these biogenic oozes than the Bolivina/
Bulimina group of species. The composition of the successive assemblages in
this lower part of the Trubi is rather variable, which seems to indicate unstable
and repeatedly changing environments. Conditions at the bottom had
not yet stabilized (cf. Brolsma, 197 5b). The larger number of cibicides
specimens in 1395 may be due to reworking, since in this sample worn
specimens are frequent as well.

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In the next higher interval the alternation of marly and indurated limestone
beds (samples 65-70) is not reflected in corresponding alternations of
two different associations. None of the species shows a rhythmic distribution
pattern that would correspond to the alternating lithology types.
The appearance of Florilus grateloupi in this interval and its occasional
presence in fairly high numbers in some of the higher samples are remarkable,
since this species is thought to be characteristic for depths shallower
than 100 m (Phleger, 1951, and Radford, 1976). It either lived in deeper
habitats than those known from the Recent or it has been transported
downslope, for which no indications are available. However, its presence
might also indicate that the depth of deposition was not far below 100 m.
Hanzawaia boueana is another shallow water species mostly recorded
in small numbers only. Van Voorthuysen (1973) mentioned up to 10% along
the Spanish Atlantic coast between 12 to 85 m waterdepth. H. boueana
might indicate a shallow depth of deposition for this part of the Trubi, but
might just as easily have arrived at the place of burial, adhering to subaquatic
vegetation because of its supposed epiphytic mode of life.
Uvigerina peregrina is most numerous in this part of the sequence, which
may be the consequence of an increased supply of clay for which this species
seems to have a strong preference (Drooger and Kaasschieter, 1958).
The presence of Cibicides bradyi, frequent in some of the assemblages,
is mentioned since this species has been relied on as an indicator of greater
depths (Wright, 1977). Its present-day bathymetrical distribution ranges
from 75 to 4000 m (d. fig. 25). Frequency distributions are recorded only
by Frerichs (1970) and pflum and Frerichs (1976). The former author found
this species in the Andaman Sea in percentages never exceeding 7%. At
300 to 400 m it reaches up to 6% of the assemblages. In the Gulf of Mexico
the latter authors recorded the preferential depths for this species to be
between 1812 and 3254 m (up to 19%). It seems questionable whether this
species is indicative of greater depths.
The peak occurrences of Golina hexagona (samples 68 and 69 and in the
laminated intervals) cannot be explained from the literature data. This
species does not prefer any particular depth and it is always rare in recent
distributions.
The scarcity of Globocassidulina subglobosa in the next higher 10 m of
more thickly bedded limestone has not been explained so far. This very
tolerant species seems to become replaced by taxa such as Siphonina bradyana
and the Pullenia group. After the introduction of considerable quantities
of the latter two groups, the faunal composition shows less drastic changes
towards the top of the section 3, at least as far as the more homogeneous

sediments are concerned. Stabilization of the bottom environment from the
levels of 71 and 72 onwards may be concluded.
This period of more stable bottom conditions was repeatedly interrupted
by periods of obviously aberrant bottom environments which roughly
correspond to the laminated units. Most of the species seem to have suffered.
The endurance of O. hexagona in these periods is remarkable. The tests of its
representatives may be flattened - the cause is unknown. The high frequencies
of o. hexagona cause the other species in the counts to be reduced to
insignificant numbers. Investigation of the small sized individuals (Brolsma,
1978, U.M.B. 17) has shown that many of these species remain present, but
the adverse conditions evidently had a dwarfing effect. This effect is even
perceptible in O. hexagona.
In between the laminated units two peaks in abundance of Nodosaria vertebralis
var. albatrossi are noteworthy. This species is most characteristic for
depths between 106 and 128 m off Southern Brazil (Pareira, 1969) but it is
also frequent to abundant between 125 and 756 m in the Gulf of Mexico
(Cushman, 1918). The presence of this species in such numbers may indicate
that the depth of deposition did not exceed 800 to 1000 m.
The fair numbers of Nuttallides rugosus var. convexus in the smaller sized
fraction may indicate depths in excess of 540 m, possibly between 600 and
700 m at which its optimum abundance of 13% was recorded in the Eastern
Mediterranean (Parker, 1958).
The latter two taxa possibly delimit the paleobathymetric range of this
part of the section to 600 to 800 m (cf. figs. 25-26). The reappearance of
the Bolivina/Bulimina group in the smaller sized fraction also seems to
indicate a change in environmental conditions. The representatives of this
group are found especially on clayey mud substrates of not too great depths;
they seem to prefer habitats shallower than 300 m. Their small size may
indicate environmental stress possibly caused by a habitat too deep for their
liking or by other unfavourable conditions.
In the next higher interval conditions seem to return to normal, i.e. just
as they do below this laminated/non-laminated part of the section. The
clayey intercalation at 2 m below the top of section 3 is of special interest.
The increased supply of terrigenous fines possibly carried in suspension the
fragile and small specimens of Hanzawaia boueana to the site of deposition
together with the small mollusc remains found in sample 107 D.
The vaguely bedded, intensely burrowed compact limestones from the
lowermost, middle and upper parts of the section all have meagre benthonic
assemblages. The samples (64, 1395, 71, 72 and 104-107) have very low
B/P ratios which possibly proves that the plankton production was very

high. It remains equally possible that benthonic life did suffer during deposition
of these homogenized limestones since the a-index of some of these
assemblages is very low (samples 64 and 104). Both processes may be valid;
acting off and on, they would give rise to similar results.
The percentage curve plotted in fig. 19 for the combined arenaceous
forms gives no additional information. The peak in sample 72 is possibly
a consequence of the small total number of specimens. These forms are rare
in the laminated intervals, and also in the smaller sized fraction. Apparently
they could not endure the extreme conditions. These extreme conditions
evidently had nothing to do with lower PH values near the bottom, which
is thought to be the major factor that favours arenaceous forms in marshes
and in the deep sea below CCD level.
The faunal composition of samples 42-45 from the middle part of the
Trubi in section 4 warrants a paleoenvironmental interpretation similar to
that proposed for the marly and indurated limestone units in the upper
parts of section 3. The presence of Siphonina brady ana, Pullenia species
and the Lagena/Fissurina group was considered indicative of stabilization
of the bottom environment already from the thickbedded interval of samples
1400 to 73. The favourable environment was maintained at the seafloor
to which terrigenous fines were periodically supplied, possibly carrying the
Hanzawaia boueana specimens to the site of deposition and favouring Bolivina
dilatata on occasional shortlived clayey substrates.
Siphonina bradyana, Pullenia species and the Lagena/Fissurina group
remain frequent elements in the homogenized, thick-bedded upper part of
the Trubi at Punta Piccola, most likely indicating continuation of the stable
environment. Together with the increase in terrigenous fines new elements
are added to the faunas. These elements, Cibicides pseudoungerianus, c.
lobatulus, H. boueana and Planulina ariminensis, are by no means typical
for deep waters. Both Cibicides species are known to be attached to plants
or substrate during life, a similar behaviour is suspected for H. boueana.
However, all four taxa are frequent in clayey environments as well. The
return of Uvigerina peregrina, observed in this uppermost Trubi interval,
may be caused by the augmented supply of terrigenous fines.
Species diversity
The number of planktonic
species per sample in section 3 varies between

10 and 16 per 300 counted individuals. In the lower part of the section these
numbers are relatively high and irregularly fluctuating. In the upper part of
the column there is a more regular fluctuation pattern (fig. 14). Fluctuations
are slight across the finely bedded, middle part of the section with its
six, sometimes silica-rich intervals, which pattern is in sharp contrast with the
curve plotted for the benthonic forms.
The slight variation of the planktonic species diversity leads to the assumption
of fairly stable watermasses throughout. Only for the lower part of
the column may the assumption of rapid changes of watermass be defended.
For the upper part of the section possible changes may be explained by the
assumption that the changes in the watermass conditions were of longer
duration and smaller intensity. No significant changes in diversity are recorded
across the laminated/non-laminated interval for which a period of high
productivity of phytoplankton and zooplankton was proposed (Zachariasse,
1978). Cita (1973, 1976) assumed strong vertical mixing in the Early pliocene
Mediterranean watermass and a lack of thermal stratification based on
faunal and isotopic evidence, which would mean expansion of only the most
tolerant species and consequently a low species diversity. One would expect
the subsequent installation of a stabilized and stratified watercolumn to
cause an increase in species diversity, but no such record can be obtained
from our counts. No variations in species diversity are recorded across the
interval of silica-enrichment either. Apparently, the increase of production
(Zachariasse, 1978) was not provoked by environmental changes that were
favourable to a larger number of species.
Distribution
of species
Globigerina apertura, G. falconensis, Globigerinita glutinata and Neogloboquadrina
acostaensis are the most abundant forms throughout section
3 (fig. 20). Globigerina nepenthes-decoraperta, Globigerinoides extremus,
G. obliquus, G. trilobus and Orbulina universa are frequent elements
in many of the samples. Globorotalia margaritae and G. puncticulata are
both present in sample 1394. The latter species shows a few scattered
occurrences throughout the section, becoming abundant in the upper two
samples. The former species may attain irregularly distributed, relatively
high frequencies, especially from the finely bedded and silica-rich units
upwards. It reaches a peak just below the sudden bloom of G. puncticulata.
In fig. 21 the numerical distribution of the most frequent species has been
reproduced graphically. All Globigerinoides species have been grouped
because of supposed ecological similarities. Globigerinoides elongatus is

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16 1 128 i 83 i 2
'2 1 20 4-4 '20 .
1 : 2 'll
I 4- 22
2 4- 140 46 8
S 20 57 ;; ! 1 1
6 '2 72 85 1
12 i ;; ! 1
3" 2 44 701 8 : 7 '2
28 7 1B 55 39 t- -- '2 I '2
---
'2 3" ~ n ~ 1 1 4'9

Graph showing the numerical distribution of the most frequent planktonic species in exposure
3 at Capo Rossello.

107A 107B 107C 107D 107E 107F 107G
16 25 13 36 27 24 18 Globigerina apertura
96 72 79 61 73 80 65 Globigerina falconensis
6 12 5 17 6 2 Globigerina quinqueloba
8 43 14 50 23 18 15 Globigerinita glutinata
32 19 38 9 12 24 24 Globigerinoides obliquus
5 1 3 1 3 2 2 Globigerinoides sacculiferus
4 3 5 4 5 Globigerinoides trilobus
4 2 Globorotalia margaritae
49 35 65 14 58 50 79 Globorotalia puncticulata
57 77 56 73 56 82 59 Neogloboquadrina acostaensis
1 2 2 1 2 9 Orbulina universa
1 3 5 4 4 2 Miscellaneous
21 11 20 34 32 8 22 Indeterminable
12 11 11 11 10 13 10 Total number of counted species
300 300 300 300 300 300 300 Total number of counted specimens
Fig. 22 Distribution chart of the planktonic species from a clayey interval of the Trubi in the top
of exposure 3 at Capo Rossello.
42 43 44 45 sa~
65 53 39 16 Globigerina apertura
52 36 57 44 Globigerina falconensis
1 2 4 2 Globigerina pseudobesa
5 4 12 1 Globigerina quinqueloba
32 45 39 46 Globigerinita glutinata
12 2 14 4 Globigerinoides elongatus
9 23 12 14 Globigerinoides obliquus
5 2 2 Globigerinoides ruber
1 2 7 6 Globigerinoides trilobus
19 35 Globorotalia margaritae
32 37 15 69 Globorotalia puncticulata
47 70 47 79 Neogloboquadrina acostaensis
2 2 3 Orbulina universa
6 6 2 8 Miscellaneous
12 18 13 8 Indeterminable
16 13 14 16 Total num ber of counted species
300 300 300 300 Total number of counted specimens
Fig. 23 Distribution chart of the planktonic species from the middle part of the Trubi in exposure 4
at Capo Rossello.

extremely rare in our Trubi material and was therefore not singled out for
its supposed affinities for cooler or deeper water (see discussion under
the chapter on the Narbone formation). The laminated intervals are indicated
by dotted horizontal bands. The selected taxa show no obvious vertical
trends, with the exception of O. universa which diminishes in relative numbers
toward the top of the section. This trend is consistent with the data
from samples 42 to 45 of section 4. No relation of the frequencies with the
laminated sediments is observed either, nor do negative or positive correlations
exist between the various species (see also Zachariasse, 1978). If one
considers fig. 21 and the range chart of fig. 20 more closely, small peaks
and lows of individual taxa are certainly significant relative to the fairly
smooth pattern of the other numbers. At first sight these aberrant values
make no sense for the interpretation of the data, for which reason no computer
analysis was carried out. Fluctuating subjectivity influences during
the observations cannot be ruled out.
No change in planktonic faunal composition takes place through samples
107 A-G. Globorotalia puncticulata is abundant in these seven samples.
Globorotalia margaritae has dwindled to insignificant numbers (fig. 22).
In this part of the section the "Kummerforms" qf some species were
counted. Specimens possessing an ultimate chamber which is of equal or
smaller size than the penultimate chamber are regarded as "Kummerforms".
According to Berger (1970) high concentrations of such forms may be
indicative of environmental stress, but may also be a consequence of selective
carbonate solution. No systematic fluctuations in relative numbers were
observed for any of the species.
The planktonic faunas from section 4 show G. margaritae to be present
in appreciable numbers in two of the samples (fig. 23). G. puncticulata
reaches maximum values in the other two samples. The presence of the
former species indicates that the biostratigraphic position of these samples
is in the lower part of the G. puncticulata Interval-zone (Zachariasse, 1975,
p.38).
G. margaritae has not been found in the uppermost Trubi at Punta Piccola
(fig. 42). G. puncticulata disappears from the numerical record above PP 1,
and Globorotalia crassaformis and G. bononiensis appear. Globigerina falconensis
is extremely abundant (up to 35%) in samples PP 3 to 5 and 7.
Fig. 21 supplies us with a picture of the vertical distribution of some
selected taxa. Most remarkable are the wide and seemingly erratic fluctuations
in the relative numbers of most of the taxa. The species composition

of the faunas remains practically the same throughout the column but many
of the oscillations for individual taxa are statistically significant. There are
no clear correlations between the frequencies of the taxa which might give
a clue to the reasons for the oscillations. The entire association seems to
indicate that water temperatures were moderately to fairly warm as indicated
by the abundance of forms belonging to Globigerina falconensis, Globigerinita
glutinata and the combination of Globigerinoides species. This latter
group of species is found in the present oceans in tropical and subtropical
regions only. Be and Tolderlund (1971) describe the other two forms from
warmer waters in transitional and subtropical areas (op. cit., p. 110, fig. 6.3).
Our data are evidently too coarse to unravel the environmental fluctuations
that caused the irregular pattern. Some combination between temperature
and nutrient supply changes may have been responsible. Anyway, it seems
likely that the physicochemical factors in the upper watermass were not very
stable. No obvious relationships with the sediment-types can be distinguished
either. The laminated sediments show similar ranges of minimum and maximum
values of the same taxon. Orbulina universa, a species said to prefer
regions with upwelling (Tolderlund and Be, 1971), does not show any relation
with the sediment. Moreover, this species seems to decrease in number
across this interval. Apparently other ecological factors prohibited its success.
None of the other species shows a consistent trend throughout the
entire column of section 3.
The lowermost 6 to 7 m of the Trubi correspond to the Sphaeroidinellopsis
Acme-zone (Cita, 1975b). The peak abundance of this species evidently
does not imply that the representatives of this genus are numerically
predominant. (cf. Cita, 1975b and our figs. 20 and 29). This must mean that
they are more numerous than in the adjacent intervals (op. cit., p. 532).
Whether or not Sphaeroidinellopsis can be considered as representing the
most conspicuous component of the faunal assemblage is truly a subjective
decision if its representatives account for no more than 3% of the fauna.
The peak abundance of Globorotalia puncticulata in the upper part of
the section is most likely an ecologically controlled event. The continuous
presence of this species, although in insignificant numbers, from the Arenazzolo
upwards, means that its potential to bloom remained if the environment
should become suitable. Apparently this happened during deposition of the
upper part of the section. Increased supply of terrigenous fines (and nutrients)
may have triggered this sudden expansion. Also, in the Arenazzolo
this species seemed to show a more regular presence in clayey intervals
(Brolsma, 1975b). Obviously, the bloom of G. punticulata in the Trubi did
not seriously affect the relative numbers of the other species as shown in

figs. 20 and 22, which possibly indicates that the water-temperatures remained
stable. The perceptible negative correlations between Globorotalia margaritae
and G. puncticulata shown in samples 104 to 107 and 42 to 45 will
remain unexplained as long as there are no clues to the particular paleoenvironments
in which each of these two competitive taxa thrived.
Paleobathymetric
estimates
The charts of figures 15 and 16 give the distribution of the benthonic
fauna. We tried to obtain a depth estimate for each species and every sample.
For this purpose the dominant species in the Capo Rossello section were
plotted in a separate diagram (fig. 17). Species present with 10 or more
representatives per sample, regardless of the total number of counted specimens,
are considered (equals 5% or more of an assemblage of 200 individuals).
The number of such taxa dominating an assemblage under these
conditions varies between 0 and 8. 31 species or groups of species appear to
be as frequent as this in one or more of the 66 Trubi samples used for this
exercise. Oridorsalis stellatus and Siphonina bradyana appear in the majority
of the Trubi samples. Nodosaria vertebralis vaL albatrossi and Globocassidulina
subglobosa have the greatest numbers (79 and 69 specimens in samples
79 and 1394, respectively).
On the basis of these selected data we tried to establish minimum and
maximum depth boundaries during deposition for each assemblage. Based
on the preferential depths occupied by the dominating species in the Recent
seas, the most probable upper and lower depth limits were estimated for the
entire assemblage (heavy bars in fig. 24). The minimum depth is defined by
the deepest upper depth limit of one of the dominating species. The maximum
depth is determined by the shallowest lower depth limit of one of
them. All these data on Recent distributions were gathered from the literature.
The author certainly does not want to give the impression that all the
literature relating to the Recent distribution of benthonic foraminifera has
been considered. Many of these depth estimates can be further extended and
refined. A compilation of the applied literature data on some of our most
common species is reproduced in figures 25 and 26.
As to the method, it must be remarked that comparison on the basis of
species names in the literature is of dubious value. It may be considered
acceptable to assume that the labels of the author himself did not change
much because of variable subjectivity in the course of the investigation. But
the recent comparison between several authors on the basis of the same
material (Brolsma, 1978, U.M.B. 17) showed such tremendous differences

5
--
4
3
2
7 - - - - - - - - -
- - - - - - - - -
5 - - - - - - - - -
- - - - - - - - -
t-.- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
5
---------- - - - - - - - - - - - - - - - - - - - - - - -
-------- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
-------- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
-------- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
4600m.
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
4600m.
4600m.
4600m.
1
-------- -
-
f-- - - - - -
4e00"i
Fig. 24 Chart showing the theoretical and more probable (heavy bars) paleobathymetric range for
each benthonic assemblage in the lower and middle parts of the Trubi in exposure 3 and 4 at
Capo Rossello. Dashed lines refer to samples too poor to furnish a fair degree of reliability,
or to less probable extensions of the depth range.

in label appreciation that additional assumptions are needed to defend our
method of paleobathymetric estimates. One is that if several names are
applied for the same species, the habitats of the different nominate species
are probably very close. Another is that errors in the comparisons are not
likely to be systematic, and conclusions from a sufficient number of species,
whether correctly labelled or not, may give a reliable estimate for the average.
Poor literature data on some of the species appeared a handicap for the
depth evaluation. It is furthermore realized that the shallower forms may
have been transported downslope thus obscuring the actual lower depth
boundaries. Only in a few cases are there indications for downslope transport.
This mechanism is considered to have had no notable influence on the
autochthony of our assemblages. Most allochthonous elements present are
thought to have arrived at the site of burial attached to drifting subaquatic
vegetation or other drifting debris. It is furthermore understood that depth
in itself is not the only controlling factor that influences foraminiferal
distributions. Murray (1973) gives the excellent example of Buliminella
elegantissima living at 550 m and 820 m in Todos Santos Bay and the Gulf
of California respectively, but not occurring deeper than 150 m off San
Diego. Obviously other factors than depth control the distribution of this
species off San Diego.
For 19 samples no depth estimates could be made due to a lack of a
sufficiently diverse fauna of frequent species (especially in the laminated
intervals and for the upper 4 samples). The minimum depth of 21 samples
is 65 m, based on the upper depth limit of Oridorsalis stellatus.Cibicides
bradyi defines the upper boundary of 9 samples at 76 to 100 m. Only 3 or
4 samples have an upper depth boundary exceeding 100 m, on account of
Eggerella bradyi with an upper depth limit at 130 m, or Dentalina subsoluta
at 105 m (LeCalvez, 1958). The maximum depth for 26 samples is placed
at 926 m based on the deepest recorded occurrence of Siphonina bradyana.
Two samples (CR 79 and 88) show a shallower maximum depth limit of
823 m based on the peaks of Nodosaria vertebralis var. albatrossi. This
species is recorded from 18.5 to 823 m in the Gulf of Mexico and Atlantic
Ocean. Deeper records of this species are as yet unknown to the author.
According to this exercise the depth of deposition of the Trubi in section
3 would be between roughly 100 and 1000 m. A shallower lower limit of
about 800 m is likely if our data concerning N. vertebralis var. albatrossi are
reliable.
A paleobathymetric interpretation of the total-fraction counts (Brolsma,
1978) appears to narrow the depth range from 100-1000 m to 550-

;.Monica
Say(32)
Todos Santos 8ay (2)
r
w.coast-C.America(4-1
-
Andam~n S~a (87)
,----
Antan:tic{6i)
Antarctic
(:5~J
FalKland
Isl.(29)
AntarctiC(30)
1 1 1 1 ---
----.
Orinoco(5)
Araya - Los
Weddell sea (65)
~rctic:(61)
Test [g os ShelF (6)
""'oFf Gironde (20)
AtLantic (27)
Scotian Shelf (79)
Atl.,antic(;rl}
11 I I
Atlantic (33)
Atlantic (27)
Scot,.:; Sea (33)
~~~oJ~)
Atlantic(53)
S••IFofMexico (33)
N.AtlantiC(13)
~rr Gironde
(QO)
Golfe de Gascogne (75)
Mediterr-anean (34)
Mare LigtAre (56)
Adriatic (505)
Golf'" di Taranto (58)
GlJlF ofGascogne (33)
Medit.!.:ranean (34)
Glolfe "'e Lion (36)
Mar-e Ligure(&6)
Adriat:ic(22)
~ic(;5)
6"011'0 di Taranto (58)
1 1
Bulimina acv/eata
9dja California (&1)
T
s.and N_Wof
---.---
LOS Testigos (6)
Orinoco (5)
~W.G\llfofMexjcO(i4)
ofF 6ironde (20)
~riti.:sh channel (to)
;.Mediter-ranean(l)
French Atlantic. coast (38)
Barent See (69)
-----.
Antarctic (30)
"11
-.-
;:eltic Sea (10)
ofFSpanish Slihara (44)
E.a"tern coast U.S. Atlantic (53)
sa}st.8rielAc (37) I
off Gironde (20)
~asCCl9"~(47)
~r:~~ean Sea(f8)
:driatiC(S&)
Adriatic (i8)
1
:d..-ia~ic (50:»
Vvigerina peregrina
I i I I I
~ 100 1000
20
oFfPrYl11ol.lth
(iO)
off" 6ironde (:20)
____ fi"esa"ds
offGjrond~(.:20)
_

N.padfic(54}
[
$. PaciFic (54)
Pacific Ocean (33)
of( Ca) i for'1 ia (80)
~cifTc(53)
Orinoco{S)
-r----
~ff" san:ra (74)
N.andS.At.I

1000 m, the latter corresponding to the lower epibathyal zone of Wright
(1977). This more restricted depth range is based, however, on the distribution
of a single species, Nuttallides rugosus var. convexus, for which only
one literature reference is available (Parker, 1958). It is moreover unlikely
that much importance can be attached to the comparison of our small
specimens with the presumably larger ones of Parker. Nevertheless we
think that the shallower part of the depth range may be excluded. If deposition
occurred at a depth of a few hundred meters only, we would expect a
greater admixture of light dependant species. By restricting the depth estimates
to 500-800 m we are well aware that we moved far beyond our
(pseudo- )quantitative analysis.
The variation in depth is rather large, some 900 m, but within these limits
it is considered a fair estimate. We learn from this excercise that no reliance
should be placed on the distribution of a single species or on a small group
of (selected) species. Cita concludes (1973) that the presence of Eponides
umbonatus, Cassidulina subglobosa, Pleurostomella alternans and bggerella
bradyi in the Trubi of Capo Rossello indicates depths beyond 1000 m (and
even as low as several thousands of meters). This seems unjustified particularly
because she advises that care should be taken with the evaluation of Decima
and Wezel's data in her footnote (op. cit., p. 216) by drawing attention
to the fact that depth is not the only controlling factor.
Samples JT 1395, CR 72, 74-77, 82-83, 86-87, 89, 94-95, 100 and
104-107 are too poor and too monotonous to give any "reliable" depth
estimate. The etched and worn part of the fauna of sample 1395 is obviously
transported to deeper environments; its well-preserved autochthonous counterpart
is typical for deeper water. The meagre assemblages of the samples
mentioned above contain a few of the dominant forms in smaller numbers.
Oolina hexagona is predominant in some of these samples (e.g. CR 75 and
77) constituting 70 to almost 100% of the assemblage. All samples from the
6 laminated intervals appear to contain very high numbers of o. hexagona
specimens in the smaller fraction (60-125 11) as shown in fig. 18. This species
is found today between 0 and 4600 m, and is always rare except for a
few frequent occurrences reported by Cushman (1918) from the Atlantic at
44 m and 90-95 m. The estimated depth for the entire section does not
strongly disagree with these depth data. The meagre or monotypic character
in the laminated intervals suggests that factors other than depth were of
importance.
The less common species such as Bulimina costata, B. inflata, Cibicides
lobatulus, Dentalina communis, Dimorphina tuberosa, Gyroidina orbicularis,
Lenticulina spp., Martinottiella communis, Melonis barleeanus, Pleurostomel-

la alternans, Sigmoilopsis celata, Sphaeroidina bulloides and Vulvulina pennatula
all have wide depth ranges which fit in well with the suggested depth
range for this part of the Trubi.
Three of the four samples studied from the middle part of the Trubi in
section 4, appear to have an upper depth limit of 76 to 100 m based on
Cibicides bradyi. Sample 42 has a shallower upper depth limit of 45 m based
on Siphonina bradyana. Three of the four samples show a maximum depth
of 926 m based on the presence of S. brady ana. Sample 45 produces a
questionable shallower maximum depth based on the presumably epiphytic
Hanzawaia boueana which may have been transported to deeper water without
suffering notable damage.
From these data no great changes in depth can be proved to have occurred
from the base of the Trubi up to at least its middle part.
A similar quantitative examination was carried out on D.S.D.P. material
from leg 42 A by Wright (1977, in press). By means of benthonic foraminiferal
species with well defined upper depth limits, minimum depth estimates
of the assemblages were obtained. "Those species representing the deepest
habitat in a fossil assemblage were assumed to be in place and those species
indicative of shallower depths were considered as possible downslope contaminates"
(pers. comm. R. C. Wright). In our study the shallowest lower
depth limit of a dominant species was used to define the lower depth boundary
of the assemblage. This was done in order to eliminate unlikely deep
(4000-6000 m) lower depth boundaries as indicated by the extremely
deep lower depth limits of some species. Wright's paleobathymetric reconstruction
shows that the minimum depth estimates of his samples surpass
our maximum values consistently by some 200 to 500 m throughout the
Pliocene of the leg 42 A cores (d. his figure of site 371). Most of the studied
core recoveries are believed to have been deposited at upper mesobathyal
depths (1000/1300-1800 m). This consistent difference between our
paleobathymetric estimates is not thought to be the result of the slight
differences in the methods (deepest versus shallowest lower depth limit)
but to actual differences in paleobathymetry. The Trubi-type limestones
recorded from the D.SD.P. sites of legs 13 and 42 A and from land (Sicily,
Calabria, Zakinthos and Crete) are considered to be facies-bound rather
than depth-controlled sediments. It is therefore quite possible that fossil
assemblages recovered from marginal areas, such as Capo Rossello, indicate
shallower depths of deposition than those from more central parts of the
Mediterranean basins. Differences of the order of 1000 m cannot be excluded.

In this respect it is interesting to evaluate a Trubi assemblage recovered
from the northern margin of the Ragusa platform near Buccheri along the
road N 124. The Trubi limestones outcropping in this area are associated
with volcanic lava intercalations, as described by Di Grande (1969). At the
Buccheri locality the Trubi contains numerous globular bodies of about
30 cm in diameter, which are composed of similar Trubi limestone and
which seem to float in an identical Trubi matrix. This sediment-type is
regarded to be result of mass-transport and rapid deposition, obstructing
any sorting to size of the transported components. During the Early Pliocene
Buccheri was possibly situated on the eastern slope of the Cattolica basin.
The sample was taken from the matrix.
The presence of both Globorotalia margaritae and G. puncticulata would
conservatively place this sample in the lower part of the G. puncticulata Interval-zone
of Zachariasse (1975). The benthonic fauna is characterized by a
Arenaceous
Anomalina helicina
Anomalina sp. indet.
Anomalinoides grosserugosus
Anomalinoides ornata
Astrononion italicum
Bolivina advena
Bolivina antiqua
Bolivina dilatata
Bolivina reticulata
Bolivina plicatella var. mera
Bolivina scalprata var. miocenica
Bolivina spathulata
Bulimina costata
Bulimina elongata var. subulata
Bulimina inflata
Cibicides floridanus
Cibicides lobatulus
Cibicides pseudoungerianus
Cibicides refulgens
Cibicides tenellus
Cibicides westi
Dentalina sp. indet.
Ehrenbergina spinulosa
Elphidium jenseni
Elphidium sp. indet.
Epistominella exigua
2
13
1
2
1
5
4
7
2
2
1
7
1
4
5
1
1
2
6
1
1
1
8
57
200
25-30
29/200
Eponidus repandus
Globocassidulina subglobosa
Gyroidina orbicularis
Gyroidina soldanii
Gyroidina umbonata
Hanzawaia boueana
Lagena spp.
Lenticulina spp.
Melonis barleeanus
Nuttallides rugosus var. convexus
Oridorsalis stallatus
Planulina ariminensis
Planularia sp. cf. P. elongata
Pullenia spp.
Siphonina bradyana
Sphaeroidina bulloides
Trifarina angulosa
Uvigerina parvula
Uvigerina peregrina
Uvigerina pygmea
Uvigerina striatissima
Vaginulina inversa
Indeterminable
Total number of counted species
Total number of counted specimens
Fisher a-index
B/P ratio
Fig. 27 Frequency list of the benthonic species encountered in sample ]T 2072 from the Lower
Pliocene Trubi near Buccheri (Siracusa).

elatively high B/P ratio (29/200) and a large number of species (57 per
200 counted specimens). The abundance of forms belonging to the Cibicides
group (61 specimens) and the Bolivina/Bulimina group (41 specimens)
is exceptional (fig. 27). Bolivina dilatata, B. reticulata and Bulimina elongata
var. subulata are the predominant elements in the latter group. Cibicides
pseudoungerianus and C. refulgens dominate in the former group. Species
such as Siphonina bradyana and the Pullenia group, which are typical in
the corresponding Trubi part at Capo Rossello, occur in insignificant numbers
in this sample. The depth of deposition concluded from this assemblage
will not have been more than 200 m. The abundance of epiphytic forms
indicates the proximity of a hinterland.
The minimum depth estimated for this biostratigraphic interval at site
371 in the South Balearic Basin ranges from 1100 to 1400 m (Wright, 1977,
in press). In our Capo Rossello section (fig. 24) a depth range from 500 to
800 m was considered most likely. In fig. 28 the paleobathymetric ranges
Fig. 28 Paleobathymetric reconstruction for three different localities pertaining to the lower part
of the Globorotalia puncticulata Interval-zone.

for this interval at the three localities are visualized. The Trubi sediments
deposited during the early part of the G. puncticulata Interval-zone seem
to have extended from outer neritic to upper mesobathyal habitats. It may
be concluded that the Trubi type of sediments were not dependent on great,
"oceanic", depths but on open marine conditions with abundant planktonic
life and a very small supply of suspended terrigenous material. Evidently,
the depth at which Trubi sediments were formed was determined by the
geographic position of the locality. Thus, it is no surprise that lowermost
Pliocene Trubi-like sediments are claimed to contain intercalations of crossbedded
and horizontally laminated beach sands (Crete; pers. comm. J. E.
Meulenkamp) .
Although it is realized that these paleobathymetric reconstructions are
based on information from benthonic foraminifera mainly in extra-Mediterranean
regions, and therefore possibly misleading, it is evident that the
intra-formational differences in depth are more valid and trustworthy
since the same methods are applied and the same subjectivity bias incorporated.
The differences in depths thus obtained for the three localities
may be real, whereas the actual depth-estimates may err by some tens to
a few hundreds of meters.
The base of section 3 practically coincides with the base of the Zanclean
stratotype section as defined by Cita (in: Cita and Gartner, 1973).
In our fig. 29 the same essential zonations published for this section are
compiled and some of Cita's samples are placed alongside our samplelog.
The section starts with the Sphaeroidinellopsis Acme-zone (MPL 1,
Cita, 197Sb). Her Globorotalia margaritae margaritae Interval-zone (MPL
2) covers the greater part of the section. The sudden peak of Globorotalia
puncticulata in our topmost two samples (106-107) is thought to correspond
to the basal part of her Globorotalia margaritaelG. puncticulata
Concurrent-range-zone (MPL 3). The occurrences of G. margaritae and
G. puncticulata in the underlying Arenazzolo sediments, considered to be
"per definition" of Late Miocene age, as well as the scattered presence
of the latter species throughout the lower part of the Trubi section, undermine
the absolute character of the zonal scheme given by Cita. The presence
of G. puncticulata in the Arenazzolo (Brolsma, 197Sa) and its scattered
presence throughout the Trubi up to the sudden bloom in samples
106 and 107 might be explained by ecological factors controlling the species'

(/)
W FREQUENCY ~ ~
...J
~'" '"
DISTRIBUTION OF Or- r- ~
-0>
CL
-
~ "i: '" r--
2: SOME SELECTED E ~. 0>
i
1"lI.~ ~ -
u
u
- ~o
"
Ct: u
- ~ "" -
2 0

near-absence and bloom. The level of sample 106 probably corresponds to
the level of the first occurrence of G. puncticulata as identified by Cita (in:
Cita and Gartner, 1973). The scattered occurrence of this taxon in the
underlying Trubi has not been described before. Such an ecologically controlled
datum level may still be applicable within a single sub-basin, but in
the extra-Mediterranean correlation to the equatorial Pacific or New Zealand,
it may be less reliable (d. Cita and Gartner, 1973, and Van Couvering
etal.,1976).
Riedel et al. (1974) described a radiolarian fauna from sample Ros 22
which they placed in the Stichocorys peregrina Zone, the oldest radiolarian
zone known from the Pliocene. A more extensive study on several samples
from the same locality (MJ 75 -1 00) revealed the presence of Spongaster
pentas in some of these samples, whereas S. peregrina was found in all samples
containing radiolaria (Riedel and Sanfilippo, 1978). It is supposed that
ecological factors controlled the presence or absence of S. pentas. Its absence
in Ros 22 has therefore no biostratigraphical value. The biostratigraphic position
of these laminated intervals must be ascribed to the next younger
S. pentas Zone (op. cit., 1978).
According to Schrader and Gersonde (1978) the frequent Thalassiosira
convexa var. aspinosa would place the laminated/non-laminated interval of
the Trubi in the Thalassiosira convexa Partial-range-zone which ranges from
the Late Miocene through the Early Pliocene. The top of this zone is defined
at the level of the evolutionary appearance of Nitzschia jouseae. The evolutionary
change from N. cylindrica to N. jouseae is concluded to be within
our interval. The third laminated bed is interpreted by these authors to
contain at least part of this gradual evolutionary change. If this "event" is
contemporaneous in the Pacific, tropical Indian Ocean and Mediterranean,
then the interval can be correlated to the "c" event within the Gilbert
Reversed Magnetic Epoch (approximately 4.3 to 4.6 m.y. B.P.).
The entry of Ceratolithus acutus is recorded in the lower part of the Trubi
(Cita and Gartner, 1973), some 6 m above the base. The appearance of
Ceratolithus rugosus is recorded some 39 m above the base at a level some
5 to 6 m below the peak of G. puncticulata. Discrepancies seem to exist as
to the absolute age assignments of the entry levels of c. rugosus and G.
puncticulata in Cita and Gartner (1973). Cita mentions 4.5 m.y. for the
puncticulata datum (op. cit., p. 536) and Gartner dates the stratigraphically
lower C. rugosus at 4.45 m.y. (op. cit., p. 545).
Ryan et al. (1974) managed to assign ages of 4.2 and 4.5 m.y. to the
G. puncticulata and C. rugosus events, respectively. Unfortunately, the errors
in the absolute datings are not traceable, which makes the following reason-

ing very hypothetical and unreliable. On the off-chance that these ages are
applicable to the "first" occurrences of the two taxa in the Capo Rossello
section, some 5 to 6 m of sediment must have been deposited in a period of
300,000 years, indicating a sedimentation rate of 1.6 to 2 cm/1000 yrs. A
similar rate of 2 cm/lOOO yrs is obtained for the lower 6 m of the section, in
between the base of the section (at 5.2 m.y.) and the entry level of c. acutus
some 6 m higher (4.9 m.y., fide Ryan et al., 1974, p. 653). The entire section
between the base and the flood-entry of G. puncticulata in sample
CR 106 would have been deposited in the course of 1 million years, which
indicates a much faster rate of sedimentation of 4.4 cm/lOOO yrs. This either
means that the rate of sedimentation must have increased dramatically
during deposition of the middle part of our section or that the correlation
of the biostratigraphic events to the radiometric timescale is unreliable, or
both. If one assumes that the correlations are correct, this means that the
middle part of the section, some 33 m in thickness, must have been deposited
in about 400,000 yrs, indicating a sedimentation rate of 8 cm/1000 yrs.
This high rate of sedimentation is not usual for biogenic sedimentation. It
can be explained, however, by either an increased supply of fine terrigenous
clastic material or by a strongly increased productivity of fauna and flora.
Although clay contents do vary in the section, the observed differences
alone certainly cannot explain the very high sedimentation rates. However,
Zachariasse (1978) showed that higher production rates of planktonic organisms
probably caused the laminated character in the 8 m thick laminated/
non-laminated interval, in which there are more clayey intervals and distinct
evidence of blooms of siliceous organisms such as radiolaria and diatoms.
The more vaguely bedded and intensely burrowed compact limestones of
the lower and upper parts of the section thus might correspond with the
periods of low sedimentation rates of approximately 2 cm/lOOO yrs., for
which the highest carbonate values are recorded (cf. Cita and Gartner, 1973,
p.527).

Fig. 30 Punta Piccola section, showing the topmost Trubi beds at the left and the overlying Monte
Narbone marls (strike and dip: 330° and 10°).

Although the top of the Trubi and the boundary interval with the overlying
Narbone unit was sampled at two localities, we preferred the Punta
Piccola section for our microscopic investigation. At Punta Piccola (fig. 1)
the outcrop is fresher (figs. 30 and 31) and the gentle dip of the strata
(330 0 _10 0 ENE) and the length of the exposure permitted the investigation
of a continuous profile of some 45 meters and provided ample information
on the lateral continuity of the individual layers.
On top of 12 m of vaguely bedded, compact Trubi limestones (samples
PP 1-7, fig. 39) the 33 m of the lower Narbone formation are characterized
by an irregular vertical alternation of blue-grey coloured marls and browngrey
to black coloured clays and clayey marls. Fourteen of these brown
coloured intervals (A-N) have been recognized. The topographic top of the
section is formed by unconformably overlying Quaternary terrace deposits
(fig. 30 and 31).
The ~ontact with the underlying Trubi limestones is arbitrarily placed at
the first brown coloured layer. The sediments still have a high carbonate
content but the cream colour of the Trubi rapidly changes to more bluegrey
and sometimes to green directly above this first brown coloured interruption.
Apart from the dark bands the lower part of the Narbone formation
resembles the Trubi, but weathering differentiates and accentuates the minor
lithological differences; the sediment gives the impression of being more
clayey. Small mollusc remains, though rare, already appear between the first
and second brown bands. From the level of sample PP 35 onwards the sediment
becomes even more clayey and mollusc remains, including small pelecypods,
are more frequent. Bioturbation, which is characteristic in the
lower 21 m, rapidly disappears from this level upwards and remains only
in the brown coloured intervals. Rounded, concretionary inclusions and
concretionary beds become frequent.
The rhythmic character of the sediment in the lower 21 m is a consequence
of the intercalations of dark, clayey marls. The mineral suite of
12 samples (18 to 29) was analyzed by means of X-ray diffraction (fig. 32).
Most of the samples contain the listed minerals in about equal proportions.

Chlorite/montmorillonite and albite show a weak tendency to increase in an
upward direction. Badly crystallized dolomite was found in samples 24 and
25 and traces of better crystallized dolomite are noteworthy in samples 27
and 29. Sample 26 is anomalous in that there is an absence of most minerals
and an abundance of gypsum and hydrated ferrisulphates. The presence of
kaoline in some of the samples was suspected but could not be substantiated
in this type of analysis. The same series of samples has been investigated
chemically. High concentrations of ferromanganese oxides have been shown
to be present in the three darker coloured intervals (E-G, fig. 33). Comparable
high concentrations of presumably cobalt and nickel, incorporated
in the iron- and manganese oxides as isomorph replacements, were also
found in these darker layers. The adjoining light green-blue marls appeared
to contain normal, low concentrations of these elements. Moreover, low
concentrations were demonstrated for zinc, copper and lead. The low values
for zinc, however, show definite peaks in the darker coloured intervals. The
concentration of copper decreases at first across intervals E and F to form
a peak in interval G, after which it decreases again to values higher than
those below. The lead concentration is uniform at 5 ppb and shows no relation
with the other elements.
The brown coloured intervals range in thickness from 10 to 130 cm, but
Fig. 31 Close-up of the boundary interval of the Trubi and Monte Narbone marls at Punta Piccola.
Dark coloured, ferromanganese-rich interbeds are indicated with A to L.

29
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27
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most of them are of the order of 15 to 40 cm. The marls in between attain
thicknesses of 30 to 200 cm. The upper and lower contacts of these manganese-rich
beds are in some cases gradational, in others sharp, but mostly
they are burrowed. Most of these beds have adjoining intervals in which
the brown coloured sediment is mixed with the green coloured marl, usually
as consequence of intense burrowing. These mixed intervals are 2 to 20 cm
in thickness. Intervals of mixed nature overlying a dark band contain at
times brown-yellow coloured concretionary inclusions similar to concretions
from the Trubi (Brolsma, 1975b). Internally the brown coloured beds may
show very rapid, irregular vertical as well as horizontal alternations of dark
and light brown colomed lenses. The lighter lenses comprise many cream
colomed, small burrows whereas darker ones contain almost none. These
small and bifurcating burrows are similar to the Chondrites from the Trubi
(figs. 34 and 35). They are often arranged parallel to the stratification and
occur in concentrations, either in other larger, darker coloured burrows or
at random throughout the sediment. The larger burrows occur primarily in
the dark clayey horizons and are usually parallel to the stratification. The
dark layers have frequently lost their internal structure completely due to
intense burrowing but may still contain ferruginous lenses of up to 30 cm
in length (sample PP 19).
The most conspicuous, manganese rich interval, G, shows a gradational
lower cant act with the underlying cream caloured clayey marl. Within 1 cm
the colour changes to brown via light brown. The lower 10 cm of this 30 cm
layer are thin-bedded with an irregular vertical alternation of light (sample
PP 25) and dark brown coloured thin beds (sample PP 24). The light coloured
thin beds actually contain very thin, small, cream-coloured streaks, often
observed in diatomites. Contacts between the thin beds are straight and sharp.
They range in thickness from 2-20 mm. The thin beds contain irregular
patches and seams of dark brown sediment. Distinct fluid-flow structures
are preserved (figs. 36 and 37). A yellow, 2 cm thick thin-bed with small
gypsum crystals forms the top of this laminated lower part (sample PP 26).
Mixing of yellow and brown material directly below this thin-bed may be
due to bioturbation. The next 20 cm are brown and show an increasing
number of burrows (sample PP 27) and ferruginous inclusions. The contact
with the overlying cream coloured marl is again gradational.
Brown and yellow caloured burrows which can be distinguished in sediments
which do not have a mottled appearance may attain a diameter of
1 cm and a length of some 20 cm. They are mostly filled with resistant
minerals such as gypsum and jarosite (cf. Brolsma, 197 5b). At about the
middle of the section small burrows of 1 mm diameter have resistant black

pyrIttc cores similar to those from the Trubi (op. cit., p. 362). The larger
burrows seem to increase in number in the upper part of the section from
the level of sample PP 35 upwards, whereas small scale burrowing disappears
in this direction, to remain only in the dark coloured intervals. The small
bifurcating burrows remain present throughout. Rounded concretionary
inclusions with yellow interior and harder brown coating increase in numbers
towards the top of the section. With diameters of 2 to 4 em they resemble
those from the Trubi at Eraclea Minoa (op. cit., p. 374). They are often concentrated
in levels and in some cases they are associated with concretionary
layers of 4 to 10 em thickness, especially in the dark coloured intervals
(e.g. the level of sample PP 36). Two of such layers were sampled (PP 37 and
49).
The clayey/marly upper part of the section comprises a remarkable 40 em
thick, yellow coloured clayey marl containing levels rich in concretions
(sample 46). The next brown coloured intercalation, 1 m above the yellow
one, contains several similar concretionary layers.
The section ends with 2 m of the regular, grey coloured clayey marl,
which is unconformably overlain by a Quaternary terrace deposit.
Monte Narbone sediments which follow stratigraphically on top of the
Punta Piccola sequence are exposed at Lido Rossello. The lithology does not
change much in an upward direction towards the unconformably overlying
calcarenitic sands. The dark clayey horizons gradually disappear. In the
upper part of the section rich and diversified pelecypod assemblages appear
which were discussed by Magne et al. (1972). At some levels the clayey marls
are sandy. In the topmost part the sediment is of very dark colour, is plastic
and contains very small molluscs. From an interval between 30 to 70 m
below the calcarenitic sands (section 6, fig. 1) 4 samples have been studied to
check whether any significant changes had taken place with respect to the
upper part of the Punta Piccola section. Samples 153 to 156 start stratigraphically
some 50 m above PP 50.
Discussion of the lithology
The presence of a hiatus or an intercalation of lagoonal sediment at the
passage from Trubi to Monte Narbone marls assumed by Magne et al. (1972)
could not be ascertained in our sections. A condensed interval (op. cit.,
p. 153) is not regarded likely either (cf. our discussion of the biostratigraphic
position of the Punta Piccola section). The lagoonal interval recorded by
Decima (1964) in core material from a bore-hole near Realmonte has not
been recognized by that author in nearby outcrops either.

The change in colour from cream to blue-grey in the lower part of the
Narbone formation may be explained by an increase in the clay content.
This idea is supported by the marly appearance which is produced by selective
weathering processes. Bioturbation is intense, indicating favourable
bottom conditions and low rates of sedimentation. If productivity of especially
the nannoplankton and planktonic foraminifera had remained
unchanged, an increasing supply of terrigenous fines must be regarded as
being responsible for the observed change. This would have led to increasing
sedimentation rates, which however, never went beyond the point at which
burrowing activity could become obstructed. Only above the level of sample
PP 35 might the sedimentation rate have become too great. It is plausible
however that production of calcareous plankton did decrease as a consequence
of repeated ecological stress. The tranquil sedimentary process was
interrupted 14 times during periods in which dark coloured, dayey to
marly sediments were deposited. The dark colours are caused by ferromanganese
oxide deposition, which probably was a relatively rapid process, as
witnessed also by the low concentrations of zinc, copper and lead (pers.
comm. C. H. van der Weijden). Regular manganese deposits contain much
higher concentrations of these elements. The metals including cobalt and
nickel, were probably supplied by brines, originating from sub-surface
volcanic activity in this area. The impact of such brines on the seawater
chemistry is recorded in an area of at least a few km 2 , because similar
bands are found outcropping at Capo Rossello. At one level within interval
G, fluid-flow structures that resemble cloud-like dispersal patterns (figs.
36 and 37) are thought to have been produced by percolating brines. These
patches have not replaced the original sediment but have stained it dark
brown, indicating the process to be "post-sedimentary". The time-lag between
deposition of the sediment and subsequent staining was short as
indicated by the Chondrites burrows which are not visibly affected by the
staining. When staining is less intense, for instance in the second interval
(B), it specifically follows the more porous paths of small burrows.
The extensive basaltic lava outflows recorded in the Pliocene along the
margins of the Ragusa platform in the surroundings of Mineo and Licodia
Eubea (Di Grande, 1969), indicate that volcanic activity locally played a
major role during the sedimentation process. This volcanic activity in the
eastern part of the Cattolica bassin may possibly be linked with the formation
of such brines.
The chlorite/montmorillonite and albite demonstrated by the X-ray
analyses might have had a volcanic origin as well (pers. comm. R. D. Schuiling).
Sub-recent oxidation by means of meteoric waters of an original

pyntlc limestone mud may have resulted in the mixture of gypsum and
hydrated ferrisulphates found in sample 26. These minerals are indigenous
and have not been transported to this site (pers. comm. R. D. Schuiling).
The presence of NaCl is probably the result of today's position of the section
along the coast.
The precipitation of ferromanganese oxides evidently did not destroy
bottom life as witnessed by the abundant benthonic foraminifera in the
dark layers. The presence of Chondrites burrows filled with the contrasting
cream colour of the overlying sediment is proof of the sedimentary nature
of the metalliferous admixtures and indicates that these beds contained
sufficient quantities of organic debris. The presence of thin-bedding in the
dark coloured interval G points to rapid deposition or less probably to unfavourable
bottom conditions during sedimentation, but both would have
prevented destructive bottom life.
Subsequent burrowing in these manganese-rich interbeds produced the
mixed intervals in which reducing conditions below the sediment-water
interface may be held responsible for the presence of brown and yellow
coloured concretions (cf. Brolsma, 1975b, p. 362). The 2 cm thick thin-bed
of interval G is probably the product of reactions between pyrite and calcium-carbonate
producing secondary gypsum and sulphur. Such circumstances
became more frequent in the topmost part of the section (levels
of samples PP 37 and 49). Similar reactions may have taken place in the
burrow-fills which contain pyrite, gypsum and jarosite. These reducing
conditions seem to have increased in intensity towards the top of the section
from the level of sample PP 35 upwards. Probably the amount of
organic debris increased, depleting the subbottom sediments of oxygen,
thus obstructing further burrowing life, as indicated by the decreasing
presence of burrows, and enhancing the formation of pyrite. The increasing
supply of terrigenous clastic fines from the level of PP 35 upwards may have
brought in the growing amount of organic debris. Mollusc-remains also
become more numerous from this level upwards, indicating flourishing
bottom life, a likely consequence of a growing supply of organic matter.
On the other hand these molluscs might also indicate a decreasing depth of
deposition.
The changes in lithology and faunal development support the idea of an
approaching hinterland which supplied the terrigenous fines and organic
material in increasing quantities. The growing number of mollusc remains
may indicate a shoaling tendency towards the top of the sequence.

The foraminiferal faunas from the Monte Narbone marls, of which 47
samples have been studied, are in a slightly better state of preservation than
those from the Trubi. Variable proportions of the faunas from the manganese-rich
sediments are dark-brown; small black spots on the tests may
occur as well. The remainder of such faunas is not coloured or coated. Apart
from the coating these faunas are well preserved. In some samples hyaline
species may have turned opaque. Pyrite may fill the tests of the assemblages
in varying degrees and proportions. In some samples broken specimens are
more abundant than in others.
B/P ratio
The B/P ratio rapidly increases in the lower part of the Narbone formation.
The number of benthonic forms per 200 planktonic specimens varies
between 4 and 41 (fig. 38). The maximum values are clearly linked to the
manganese-rich intervals though some of them (E, I, Land N) show hardly
higher or even minimum values. The lack of fauna in sample 26 and especially
in sample 37 is probably due to post-sedimentary dissolution. The small
numbers in 26 probably come from adjoining lamina that were incorporated
in the sample.
The top four samples from the Narbone formation at Capo Rossello contain
a very rich benthonic fauna with a maximum of 48 specimens per 200
counted planktonic individuals in the topmost sample (figs. 38 and 40).
The increasing B/P ratio across the boundary between the Trubi and the
Narbone marls (fig. 38) may indicate that the planktonic production decreased.
On the other hand increased B/P ratios might also have resulted
from the increasing success of benthonic life because of an improving bottom
environment; this alternative provides an equally good explanation.
Just prior to periods of oxide-precipitation favourable bottom conditions
seem to have enhanced the productivity of the benthonic foraminifera, as
suggested by the consistent peaks in the ratios at these intervals. It is theoretically
possible that planktonic life suffered from the effects of supposed volcanic
activity, thereby causing relative blooms in benthonic forms. However,
ecological stress does not seem to have affected the number of planktonic
species (fig. 38).

The sharply increased B/P ratio in the upper four samples at Capo Rossel-
10 would be in agreement with the inferred shallowing tendency.
Species diversity
The Fisher

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posite- reactions with higher a-values. Samples 24 and 27 from the lower and
upper parts of horizon G show relatively high a-indices (14 and 16). Sample
25 is very poor in species (only 10), whereas sample 49 is very poor in specimens
(fig. 39). Post-sedimentary dissolution may be held responsible for the
lack of fauna in samples 26 and 37. It is to be noted that ferromanganeseoxides
have been demonstrated in only a few of the darker grey-brown
coloured levels (E-F -G); it is only assumed that all other dark coloured intervals
have similar high concentrations of manganese, iron, nickel and cobalt.
Diversity diminishes in the upper four samples (fig. 38).
Arenaceous
Bolivina spp.
Bulimina elongata var. subulata
Cassidulina laevigata var. carinata
Cibicides bradyi
Cibicides tenellus
Cibicides pseudoungerianus
Cibicides lobatulus
Eggerella bradyi
Gyroidina umbonata/orbicularis
Hanzawaia boueana
Lagena spp./Fissurina spp.
Oridorsalis stellatus
Planulina ariminensis
Pullenia spp.
Quinqueloculina spp.
Sphaeroidina bulloides
Uvigerina peregrina (incl. parvula)/pygmea
Uvigerina proboscidea
Bulimina spp.
Cibicides refulgens
Globocassidulina subglobosa
Gyroidina soldanii
Gyroidina parva
Lenticulina spp.
Me Ion is barleeanus
Oridorsalis umbonatus
Miscellaneous
Indeterminable
Total number of specimens
Total number of species
Fisher a-index
Number of benthonics/200 planktonics
Fig. 40 Distribution chart of the benthonic species in the upper part of the Narbone formation at
Capo Rossello (exposure 6).

The lower O'-indices in most of the darker intervals are caused by the
abundance of a single species, Bulimina aculeata. In intervals Band F this
species is rare or absent, a fact which accounts for the more regular 0'-
values. An extreme example of low O'-value is sample 25 in which a very
large number of specimens of only 10 species cause a high B/P ratio.
According to Murray (1973) such low O'-values of 2-3 are indicative
of lagoonal and restricted, nearshore environments, marshes, bays and
estuaries. It is unlikely that such environments played a role in this instance,
but the low values show the severity of the ecological stress.
From these data we have to conclude that at the approach of periods
of manganese-enrichment and immediately after such periods, the quality
of the bottom conditions was good. During the acme of such enrichment,
conditions at the bottom were usually appreciated by fewer species but
in relatively greater numbers.
The predominance of a few taxa in the upper four samples with supposedly
shallower affinities, e.g. Cassidulina laevigata var. carinata and Cibicides
pseudoungerianus, is responsible for the decreasing diversity.
Distribution
of species
Cibicides pseudoungerianus is one of the most frequent species encountered
throughout the section (fig. 39). Bigenerina nodosaria, Cibicides bradyil
Cibicides robertsonianus, Eggerella bradyi, Planulina ariminensis, Pullenia
spp. and Uvigerina peregrina are present in most of the samples in appreciable
numbers. Siphonina bradyana shows an irregular decrease in frequencies
towards the top of the section. A group of more or less successful
species of the Trubi are present in most of the marly samples but in smaller
quantities than before: Globocassidulina subglobosa, the Gyroidina species,
Oridorsalis stellatus, O. umbonatus and Karreriella species. The fairly common
Trubi species Cibicides italicus rapidly disappears from these more
clayey sediments.
Most interesting, however, is the appearance of new taxa from the second
dark coloured interval upwards. Bulimina aculeata, Bulimina exilis and
Epistominella smithi are most conspicuous (fig. 41). The first species forms
almost 50% of the fauna in the dark-coloured interval D, and reappears again
in level H forming 40% of the assemblage. In an upward direction all peak
abundances of this species occur in the manganese-rich intervals. B. exilis
has only been recorded from the manganese-rich interval G, especially in
sample 25, in which it constitutes 46.5% of the assemblage. In the same
interval E. smithi appears as 22% of the fauna. It is almost the only species
in the next higher sample and does not recur in the overlying sediments.

------ Cibicides lobatu(us
-- Hanzawaia. boueana
............. Planu(ina ariminensis
_.-.-.- Cibicides pseudoungerianus
EJ Bu(imina aculeata
~ Bulimina. exilis
EIm Epistominfl/{a
smithi

------ Cibicides lobatu/us
-- Hanzawaia boueana
............. Planu/ina ariminensis
_.-._.- Cibicides pseudoungerianus
EJ Bulimina aculeata
~ Bufimina exilis
[JJ Epfstomin&lIa
smithi

Bulimina inflata, Hopkinsina bononiensis and Bolivina alata are first recorded
in the upper part of the section and they too reach relative peaks in
the manganese-rich intervals (fig. 39).
Uvigerina parvula has been counted together with Uvigerina peregrina. No
vertical trends or correlations with the lithology are shown by either of.
the two species.
The change from the biogenic carbonate deposition of the Trubi to a more
clayey sedimentation in the Narbone formation is reflected in the concurrent
change in faunal composition. Species, characteristic for the Trubi, diminish
in numbers towards the top of this formation (called Trubi-runners in fig.
48). Other species or groups of species increase in abundance in the same
direction, e.g. the epiphytic species (from 2-7% in the Trubi to 17-23% in
the Monte Narbone marls, fig. 48).
Cibicides lobatulus, c. pseudoungerianus, and Hanzawaia boueana are the
most conspicuous epiphytic elements. The epiphytic habitat of the latter
species is not known from observations on Recent material but suspected
on the basis of its concavo-convex morphology and its preference for shallow
waters. C. pseudoungerianus occurs in coarser sands of the outer part of the
Orinoco shelf (Drooger and Kaasschieter, 1958), on muddy substrates from
shallow to bathyal environments in the Mediterranean '(Blanc-Vernet, 1969),
as sessile forms between 0 and 660 m near the Falkland Islands (Heron-Allen
and Earland, 1932), with fixed habitat on calcareous mollusc debris at 20
to 60 m water-depth in the Bay of St. Brieuc (Dupeuble et al., 1971), or as
epiphytic forms in the inter- and forereef facies of Barbuda where coarse,
angular carbonate sands or Homo trema-sands form the substrate (Brasier,
1975). This species is also recorded from clayey substrates in the Barentsz
Sea with highest frequencies at 350 m (Jarke, 1960) and in the Andaman
Sea at 800 to 1000 m and 1600 to 1800 m (Frerichs, 1970). Cibicides
lobatulus is also a species living fixed to vegetation as well as free in the
sediment of the Mediterranean (Blanc-Vernet, 1969). The depth ranges of
both species is shown in figs. 25 and 26, respectively, from which it appears
that both may live in shallow to moderately deep waters (down to 500 m,
reported sometimes as deep as 4000 to 5000 m). The recent distribution of
Hanzawaia boueana is not well-known. All available records indicate the
species' preference for shallow water. Highest frequencies (up to 10%) have
been described from water shallower than 85 m along the Spanish Atlantic
coast (van Voorthuysen, 1973).
The high percentages of this group of epiphytic species may indicate
the proximity of vegetated areas. Such areas today have depths not exceeding
50 m because sunlight, needed for photosynthesis, must be able to reach

the bottom-bound vegetation. It should be borne in mind that this entire
group may represent an allochthonous constituent of the assemblage. The
greater abundance of the group may therefore be indicative of increased
transport from coastal areas. The relatively higher marl and clay contents
throughout the section certainly point to an increased supply of terrigenous
clastic fines which could have carried along drifting submarine vegetation
with the adhering epiphytic fauna to the area of deposition at our more offshore
locality.
The depth-ranges of the other species which are reported to occur in
appreciable numbers in most of the samples are shown in figs. 25 and 26.
Bigenerina nodosaria is a species living in fine muddy sediment (LeCalvez,
1958) as well as in fine and coarse sands (Pujos, 1971, and Mathieu, 1971).
Depth ranges are the only data available for Cibicides bradyi/G. robertsonianus.
This latter species, which appears to be a morphological variant
of the former (see also pflum and Frerichs, 1976), prefers bottoms in excess
of 155 m depth and it is most abundant between 600 and 1100 m in the
Gulf of Mexico (Phleger, 1951, and Parker, 1954). All available data on
Eggerella bradyi concern depth; other environmental information has not
been found. Planulina ariminensis, a dominant outer shelf species in Baja
California (Bandy, 1961), shows a peak abundance in the Gulf of Gascogne
between 900 and 1200 m; this is thought to be related to oxygen minima
and increased salinities (Pujos, 1970). It is found living in clays and clayey
sands between 270 and 1120 m off the Sahara coast (LeCalvez, 1972). The
Pullenia group of species, comprising quinqueloba (including quadriloba),
bulloides and salisburyi, is present at every latitude and at almost every
depth (Cushman, 1918). According to Cushman, P. quinqueloba and P.
bulloides prefer deeper and cooler waters. Uvigerina peregrina is found living
at 1 to 20 m and between 30 and 40 m in waters surrounding Tobago Island
in frequencies of 1 to 5% (Radford, 1976). It forms 15 to 24% of the assemblages
at depths greater than 1100 m in the Gulf of Gascogne (Caralp
et al., 1970). Relative high frequencies are reached down to 1600 m in the
N.E. Gulf of Mexico (Parker, 1954). This species is known to live in fine and
coarse sands (Pujos, 1971) and may reach up to 81% of the assemblage in
pelitic sediment off the Orinoco where it is independant of depth, avoids
salinity fluctuations and is supposed to be a true mud-feeder, according
to Drooger and Kaasschieter (1958).
Bulimina aculeata appears to be the most successful species in most, but
not all manganese-rich levels. The bathymetric distribution of this taxon
(fig. 25) is wide, as it is reported from 1 to 4700 m. In the Gulf of Mexico
it seems to prefer depths between 500 and 2000 m (Phleger, 1951, and

Parker, 1954). In the Andaman Sea this species forms 50% of the assemblages
between 300 and 400 m (Frerichs, 1970). In the Gulf of Taranto
highest frequencies are reached at a depth of 100 m (Iaccarino, 1969) and in
the Adriatic its greatest abundance was recorded at 26 to 27 m and at 32 m
(Iaccarino, 1967). Blanc-Vernet (1969) describes this species from the
French Mediterranean coast as an abundant form occurring in coastal and
bathyal clays from 40 to 50 m downwards and increasing in abundance
with depth to 300 m. In the Atlantic this form is reported to be abundant
at 90 to 105 m and 180 to 210 m (LeCalvez, 1958) and in the Antarctic
it is abundant at 870 m and 1900 m (Uchio, 1960). The species lives in fine
sands (Pujos, 1971) off the Gironde. In the Gulf of Lion it occurs in waters
shallower than 20 m and is described to be euhaline (S = 30-40 gll, Levy,
1971). Barbieri and Medioli (1969) recorded this species from the Scotian
shelf on sandy bottoms, though in small numbers, between 38 and 145 m.
This taxon is not successful in all manganese-rich intervals. In the most
conspicuous interval G it appears to be entirely absent. Another Bulimina
species, B. exilis, has taken its place. This species is entirely restricted to this
interval G, especially to the level of sample 25. This species is by no means
rare in deep waters (Cushman, 1918) but it seems to be temperature controlled,
living between 2000 and 2300 m off California in waters of 1.9 to
2.2°C (Bandy, 1953), whereas it is also recorded in shallow (54 m), cold
Arctic waters off the East Siberian Coast (Todd and Low, 1966). All available
data concerning its present-day distribution in the oceans are shown in
fig. 26.
It seems likely that none of the depth and temperature data are of great
importance for the flood occurrences of these Bulimina species. Probably
there is some other factor that defines the peak values. The fact that such
species may become similarly frequent prior to the Messinian salinity crisis
(Cita, 1973) leads to the assumption that the metalliferous "brines" may
have temporarily disturbed the salinity of the bottom waters. A further
consequence might be oxygen depletion because of the precipitates. Neareuxinic
bottom conditions seemed to have played a role in the Early Messinian
as well (op. dt., p. 208; Di Napoli Alliata, 1964; Salvatorini, 1968). In
Italian pre-evaporitic marls other representatives of the Bolivina/Bulimina
group are associated with the oligotypical Bulimina aculeata assemblages,
amongst which Bolivina dilatata is frequent.
The representatives of Bolivina dilatata are also capable of coping with
worsened bottom conditions. This species forms an important faunal element
in laminated sediments of the Santa Barbara basin, which are deposited
in low oxygen environments (Harman, 1964; Barbieri and Medioli, 1964). Its

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athymetric distribution is shown in fig. 26.
Epistominella smithi forms the third abundant species in interval G. All
representatives of this species appear to have undergone some mechanical
erosion as evidenced by broken-off parts on the tests, and may well form an
allochthonous constituent of this oligotypical assemblage. Murray (1973)
regards this species to be a reliable indicator of depths between 365 and
1100 m off the Californian coast. The irregular morphology of the spiral
side and its plano-convex to concavo-convex shape suggest a possible adhering
mode of life (see also fig. 26). This species is also found in Upper
Miocene, laminated sediments of Southern California which are regarded
to have been deposited in low-oxygen environments (Harman, 1964).
Other species which are introduced in the top of this section, showing
a preference for the brown-coloured intervals, are Bulimina inflata and
Bolivina alata. The former species is widely distributed in comparatively
deep water, especially in Globigerina-oozes (232-3125 m, Atlantic Ocean,
Cushman, 1918). In the Gulf of Gascogne it is recorded below 1500 m
(Wright, 1977). Bolivina alata is found living at 570 m in clays off the
Sahara coast (LeCalvez, 1972). It does not exceed the 0.2% in assemblages
recovered from the Gulf of Gascogne between 560 and 3200 m (Caralp
et al., 1970). Iaccarino (1969) describes this species trom between 10 to
610 m in the Gulf of Taranto, where it reaches up to 18% of the fauna at
610 m of water-depth, preferably living at depths exceeding 100 m.
No data are available concerning the distribution of Hopkinsina bononiensis
in the recent oceans.
Planktonic foraminifera
The planktonic foraminiferal faunas from the Monte Narbone marls
are generally well preserved. Brown coating may obscure some of the details
on the tests in the manganese-rich sediments, especially at the level ofpp 15.
The amount of broken specimens is low except in the latter sample.
Species diversity
The number of planktonic species per 300 counted individuals varies between
approximately 12 and 18 (fig. 38). Only in samples 26 and 37 is the
number very low, probably as a consequence of post-sedimentary dissolution.
No significant fluctuations are seen across the manganese-rich intervals,
a behaviour similar to that observed for the laminated/non-laminated alternation
at Capo Rossello. In the upper part of the Narbone formation the
species diversity is somewhat lower (12 to 13) and only 9 species are record-

ed from the uppermost sample (figs. 38 and 43).
From the diversity log it appears that diversity did not fluctuate much
because of the occasional dominance of a single species, Globorotalia bononiensis.
The precipitation from metalliferous solutions may have influenced
the planktonic foraminiferal production, as might be concluded from the
high B/P ratios, but there is no proof for this assumption.
In the topmost sample 156 the B/P ratio reaches its maximum value,
whereas the plankton diversity drops to the small number of 9. These data
suggest increased ecological stress in the water-column and more favourable
conditions at the bottom (a = 12). These observations may be explained by
a smaller depth of deposition, which diminishes the size of the ecological
niche for planktonic life and favours benthonic productivity.
154 155
40 2
70 92
5 65
88 29
28 36
19 16
1 3
21 30
14 9
3 15
4
2 2
5 1
300 300
12 12
~
Globigerina
Globigerina
apertura
falconensis
Globigerina quinqueloba
Globigerinita glutinata
Globigerinoides elongatus
Globigerinoides obliquus
Globigerinoides ruber
Globorotalia bononiensis
Globorotalia subscitula
Neogloboquadrina acostaensis
Orbulina universa
Globigerina bulloides
Globorotalia crassaformis
Miscellaneous
Indeterminable
Total number of counted specimens
Total number of counted species
Fig. 43 Distribution chart of the planktonic species in the upper part of the Narbone formation at
Capo Rossello (exposure 6).
Distribution of species
In fig. 44 the numerical distribution of some selected species has been
reproduced graphically. The manganese-rich intervals are shown as dotted
horizontal bands. The 4 samples from the upper part of the Narbone formation
at Capo Rossello are in the top of this figure.
An obvious relation between sediment and faunal distribution is demonstrated
by Globorotalia bononiensis. Maximum percentages are recorded

in the manganese-rich interbeds (B to E and G to J). Interval F is the only
dark layer within the range of this species from which it is missing (sample
21). It is abundant however in the directly underlying normal grey-coloured
marl of sample 20. Abundances up to 50% are reached in interval G. Due to
these very high percentages most other species in these intervals show frequency
drops. G. bononiensis appears and disappears from the record, and
its high frequencies form true acmes.
With the exception of Globigerinoides elongatus, all Globigerinoides
taxa have been entered as a single group for supposed ecological similarities.
This group is fairly common throughout the section but in general there
seems to be a fluctuating decrease in numbers to the fairly small quantities
in the upper four samples (153-156) at Capo Rossello. It is remarkable that
this group shows irregular small peaks in the higher manganese beds K-N
after the disappearance of G. bononiensis. G. elongatus seems to show a
slight increase from bottom to top to reach a peak abundance in sample
153.
Globigerina quinqueloba is another species which seems to show some
irregular increase in numbers in an upward direction. Peaks occur in both
types of sediment.
Globigerina bulloides is peculiar for its sudden bloom of about 20% in
sample 35. From this level upwards this species is somewhat more frequent
than it was below, but its frequency does not extend beyond 6%.
The number of specimens of Globigerina falconensis tends to decrease
through the topmost Trubi and into the lower Narbone formation. It is this
species which shows a peak in the dark unit F from which G. bononiensis
is missing. In the widely fluctuating pattern higher up, the peaks avoid the
dark layers.
Globigerina apertura reaches a maximum in interbed I to decrease in
abundance towards the top of the section. This trend seems to continue
towards the top of the formation (samples 153 to 156).
Globigerinita glutinata and Neogloboquadrina acostaensis are frequent
elements in many of the samples but do not seem to show vertical trends.
Minimum values for both species are related to the various peaks of G.
bononiensis. Globigerina pachyderma-types, incorporated in the acostaensis
group, occur from the level of sample 43 upwards (fig. 42).
Globorotalia crassacrotonensis and Globorotalia inflata show subsequent
appearance levels and do not recur in the topmost four samples at Capo
Rossello. The highest percentages of both species are in the regular, grey
coloured marls.

~
'53
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D 17
16
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An obvious relation exists between the peaks of Globorotalia bononiensis
and Bulimina aculeata (cf. figs. 41 and 44). Both species show a definite
preference for darker sediments supposedly rich in ferromanganese-oxides or
rather a tolerance for the environmental factors that caused these sediments.
It is likely that the same or related ecological factors simultaneously influenced
foraminiferal life at the bottom and in the overlying water column.
However, there are several deviations from the general picture. Both
species are not met with in internal F (sample 21) in which these oxides are
recorded in increased, though not dramatically higher, quantities (fig. 33).
B. aculeata is also missing from intervals A, C, E, G and I, in which G.

50
1~N
47
46
45
43
4 M
42 L
41
4
39
38
37
36 J
35
34
33
32 I
31
29
28
27
~~ G
24
23
22
21 F
20
19 E
18
17 0
16
15 C
14
13
W
B
'0
9
8 A
7
6
5
4
3
2 ,
Fig. 44 Graph showing the numerical distribution of the most frequent planktonic species at Punta
Piccola and in the top part of the Narbone formation in exposure 6 at Capo Rossello.
bononiensis does show higher frequencies. In interval G its place is taken by
Bulimina exilis. Above interbed K we lose control, because G. bononiensis
disappears from the column, possibly as a consequence of evolution. During
deposition of intervals A, C, E and I some ecological factor influenced
planktonic life in the watercolumn causing the relative expansion in numbers
of G. bononiensis, while bottom-life seems to have remained unaffected. It
seems, for instance, that during deposition of interval C, properties of the
water column (or its upper part) changed, the effect of which extended to
the bottom as late as during the deposition of the sediment of the following
interval D, eventually supporting the expansion of B. aculeata. Although it

seems reasonable to hold the addition of metalliferous solutions responsible
for the changes in the water-column, it is clear that not all periods of precipitation
from such solutions show indications in the faunas, e.g. in interval F
(sample 21). Moreover, the peak of G. bononiensis in the directly underlying
level of sample 20 suggests again that the chemical changes occurred
prior to the ferromanganese precipitation in interval F, which left the
bottom fauna unaffected. These anomalies might be explained by variable
concentrations and durations of the chemical admixtures.
The ferromanganese-oxides also precipitated on the foraminiferal tests.
Such coatings have not been observed in the under- and overlying grey marly
sediments, once again indicating the almost synsedimentary nature of the
process. The large numbers of broken specimens in sample 15 are not understood;
they may be due to rough handling during the washing and sieving
procedure of the sample.
The sudden bloom of Globigerina bulloides in sample 35 and the subsequent
entry of Globorotalia inflata in sample 38 seem to indicate decreasing
water-temperatures. In the present oceans both forms prefer cooler water.
The latter taxon is regarded an excellent indicator and the only indigenous
species of the Northern and Southern Transition Zones (Be and Tolderlund,
1971, p. 119). G. bulloides is a dominant species in subarctic and subantarctic
waters. It has a wide distribution and is common in transitional and
antarctic waters (op. cit., p. 119). Globigerina quinqueloba, which also
shows an upward increase tendency, occurs especially in subarctic and subantarctic
waters, but it is also frequent in arctic, antarctic and transitional
waters (op. cit., p. 115). At lower latitudes the latter two species may remain
frequent below the thermocline.
The combined Globigerinoides taxa include some forms that today prefer
warmer water: G. sacculiferus, G. ruber and G. trilobus (cf. Cifelli and
Smith, 1974; Reiss et al., 1974). The two extinct species, Globigerinoides
obliquus and G. extremus, are generally regarded as tropical-subtropical
forms. This group seems to decrease in numbers in the higher part of the
Punta Piccola column. Globigerinoides elongatus was singled out for its
opposite trend. It shows a slight increase towards the higher levels and
reaches a peak in sample 153. According to Hecht and Savin (1970) Globigerinoides
ruber phenotypes with a diminutive final chamber point to
isotopic temperatures 1 to 4.5°C colder than the phenotypes with a normal
final chamber from the same samples. This small final chamber was found to
be flattened in the sample with the greatest temperature difference. These
forms may well resemble our G. elongatus specimens. According to these
authors the environment of this form must be the deeper, colder water.

Emiliani (1974) analyzed core material from the Eastern Mediterranean
isotopically and found environmental changes across the glacial/interglacial
cycles to be reflected in the morphology of the shells of G. rubra populations.
His G. rubra rubra types (corresponding to our G. ruber) were found
to be restricted to warmer periods and the G. rubra gomitulus types (corresponding
to our G. elongatus) are predominant at lower temperatures.
These latter types are small, very compact specimens with very small openings
(op. cit., pI. 1, 42 cm and 182 cm; pI. 2, 382 cm, 602 cm and 708.5
cm). These observations fit in perfectly with the observed trend in our section.
The assumed cooling tendency obviously favoured the development of
the smaller compact specimens belonging to G. elongatus. Although Globigerina
falconensis is described as being an ecophenotypic variant of G. bulloides,
occurring especially in subtropical waters (Be and Tolderlund, 1971,
p. 119), no obvious trend is recorded from bottom to top. Therefore we did
not add this taxon to the Globigerinoides species group that is considered
to indicate warmer water. G. bulloides, G. quinqueloba and Globorotalia
inflata were combined to form a group with cooler water preference.
The relative proportions
of these two groups (R = ---'!!-), shown in fig.
W+C
45, demonstrates that the cooler taxa increase strongly from the level of
sample 33 upwards. The occasional peaks of the warmer taxa do not interfere
with this overall tendency which remains clearly perceptible. These
peaks seem to coincide with dark layers. The picture obtained from the
4 samples of the upper part of the Narbone formation possibly indicates a
cyclic nature in the temperature variation. The appearance of pachydermatypes
from the level of sample 43 upwards corroborates very well the assumption
of a cooling trend.
A similar picture might be obtained if depth of deposition increased. As
discussed above, however, depth of deposition is thought to have decreased,
thus supporting the assumption that water-temperatures near the surface
were indeed lowered.
This interpretation finds strong support in the work of Magne et aL
(1972) who recognized the immigration of classical cold malacofaunas, often
cited from the Mediterranean Quaternary, into the upper part of their "zone
a inflata". Their Realmonte section practically coincides in its upper reaches
with our section 6 from which samples 153 to 156 were derived. From the
level of their sample 20322 upwards they recorded Astarte sulcata, Lucina
borealis and Natica montacuti which are found in Pliocene deposits in
England and inhabit the North Atlantic Ocean today. Accordingly they
suggested that this upper part of the section, between their levels 20322 and

Graph showing the relative proportions of individuals of warmer and colder taxa throughout
the section of Punta Piccola and the toppart of the Narbone formation at Capo Rossello
(exposure 6). Dotted signature indicates proportion of warmer taxa, including all Globigerinoides
species, but excluding G. elongatus. Colder taxa include G. bulloides, G. quinqueloba
and G. inflata.

20323, was deposited at the transition from the Pliocene to the Pleistocene
in a progressively cooling and shallowing sea (op. cit., p. 154).
Ciaranfi and Cita (1973) conclude that some of the most significant
climatic changes or fluctuations in the later part of the Upper Pliocene took
place between about 2.6 - 2.1 m.y. B.P. An age of 3 m.y. B.P. has been
assessed for another distinct period of relatively cold or cool climate, which
would correspond to the base of the Nebraskan (as recorded in the Gulf of
Mexico). This event is furthermore correlated with the onset of ice-rafted
detritus in the North Atlantic and with the middle Villafranchian fauna
(op. cit., p. 1398).
Most interesting, however, is the entry of Globorotalia inflata at the onset
of cooler conditions. Again it seems likely that ecology controlled the
appearance level as was suggested before for the Globorotalia puncticulataentry.
Paleobathymetric
estimates
In figures 39 and 40 the distribution of the benthonic fauna is reproduced.
These distribution charts are considered to be sufficiently clear in themselves,
and the dominant forms have not been singled out in a separate
diagram. The number of forms dominating an assemblage (i.e. 10 or more
specimens per sample) varies between 1 and 9. 37 species or groups of
species appear with this frequency in one or more of the 50 Punta Piccola
samples.
The upper depth limit of 23 assemblages in this section lies approximately
between 40 and 50 m as is indicated by the deepest upper depth limits of
Planulina ariminensis and Siphonina bradyana (fig. 46). Seven assemblages
indicate a minimum depth of 76 to 100 m as shown by the deeper upper
depth limit of Cibicides bradyi, whereas 10 assemblages must have lived
deeper than 130 m, according to the still deeper upper depth limits of
Eggerella bradyi and Gyroidina orbicularis. Samples PP 25 and 26 are characterized
by the abundance of Epistominella smithi, a species which is reported
living today between 365 and 1830 m (combined depth estimate, fig. 26).
Samples 37 and 49 are too poor.
The maximum depth of deposition is indicated for 22 samples by the
deepest recorded occurrence of S. bradyana at 926 m, which means that all
other dominant forms in these samples have deeper lower depth limits. In
view of the distribution of Cibicides lobatulus eight out of these 22 samples
might have a somewhat shallower maximum depth of 870 m. The lower
depth limit of Hanzawaia boueana possibly indicates that thirteen of these
22 samples might have a still shallower maximum depth of 510 m. Since

4 200 ṃ
N 0
FA U N A
- - - - -
- - -
-- - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - ~~
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - -
5200 m
------ --
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - -
N 0 FA U N A
4 300 4 700 ṃ
- - - -
- - - - - - - - - - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - - - - -
4
_. 020 m
- ---------- -- .
- - - - -
- - - - - - - - - - - - - - - - - - - - - - - -
- - - - - - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - -
- - -
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - - -
- - -
- - -
---- ------ ------ --
- - - - - - - - - - - - - - - - - - - - - - - - - - - -
--
4 000 m
-
- - -
- - -
- - -
- - -
- - -
- - -
-
-. -----
Chart showing the theoretical and more probable (heavy bars) paleobathymetric range for
each benthonic assemblage in the Punta Piccola section and the upper part of the Narbone
formation at Capo Rossello (exposure 6). Dashed lines refer to samples too poor to furnish
a fair degree of reliability, or to less probable extensions of the depth range.

it is realized that the latter two species may have had an epiphytic habitat,
it is more sensible to rely on Siphonina brady ana. For the 28 samples in
which this species is less frequent than 5%, lower depth limits are much
deeper. Eight of these samples show a maximum depth of 3800 m based
on the dominance of Uvigerina proboscidae. Bigenerina nodosaria places
the maximum depth of 4 samples at 3000 m. The maximum depth of
sample 25 is approximately 850 m, according to the recent distribution
of Bolivina dilatata. [n sample PP 26 the distribution of Lpistominella
smithi defines the upper and lower depth boundaries at 365 and 1850 m
respectively. However, all forms belonging to this species appear to be
mechanically eroded, with parts of the test broken off and missing, which
may indicate a certain amount of transport. The recent distribution of
Bulimina costata indicates for sample 44 a lower depth boundary at 850 m.
The abundance of forms in this sample belonging to Bulimina and Bolivina
is believed to be dependent on the clayey substrate rather than on depth.
A number of taxa show preferential depth distributions. By means of
some of these taxa a more likely depth estimate is constructed (heavy
bars in fig. 46). [t appears that most assemblages have lived, according
to this latter method, between 100 and 400 m. This estimate is based on the
preferential depth of especially Cibicides pseudoungerianus and Planulina
ariminensis and to a lesser degree on Bigenerina nodosaria) Bulimina aculeata,
B. exilis, Globocassidulina subglobosa, Lenticulina spp., Uvigerina
peregrina, U. proboscidea and the epiphytes.
The four samples from the upper part of the Narbone formation at Capo
Rossello contain assemblages which seem to support the inferred upward
decrease in depth of deposition. The dominance of forms belonging to
Cassidulina laevigata var. carinata in the upper two samples must be mentioned
in this respect. Representatives of this species today prefer depths
of between 100 and 200 m (Caralp et al., 1970; Phleger, 1951).
The method applied to obtain these paleobathymetric estimates is not
regarded as very reliable. Other, independent lines of evidence are definitely
needed to support any clue or indication that might be suggested by such a
type of exercise.
BIOSTRATIGRAPHIC POSITION PUNTA PICCOLA SECTION
In our figure 47 the major zonations are compiled and some of Cita's
samples (197 Sa) are fitted into our sample-log. The basal part of the Punta
Piccola section is formed by 12 m of the uppermost Trubi limestones. Within
these limestones our counts record the disappearance of Globorotalia punc-

ticulata and the appearance of Globorotalia bononiensis, in sample 1 and 6
respectively. The zonal boundary between the G. puncticulata Interval-zone
and the G. bononiensis Interval-zone is tentatively placed between samples
5 and 6 (cf. Zachariasse, 1975). It is very possible that G. bononiensis
appears at a lower level but did not figure in our counts due to its original
scarcity.
Magne et al., (1972) studied the Trubi limestones and the Monte Narbone
marls from a nearby section at Realmonte. They placed the lithological
boundary between both units at a bituminous, dark coloured interval from
which their sample 20307 was taken. Directly below this dark layer the first
occurrence of G. bononiensis was recorded in their sample 20306, which
marks the lower boundary of their G. bononiensis Subzone (G. margaritae
Zone). In their sample 20308 directly overlying the dark coloured interval,
they found the first Globorotalia crotonensis and Globorotalia crassula
which define the lower boundary of their G. crotonensis/G. crassula Zone.
This would imply a very condensed interval for their G. bononiensis Subzone.
For this reason they suggest a hiatus at this point, which would agree
well with Decima's suggestion (1964) of a brackish interval at the boundary
between both lithological units, observed in a drilling at Realmonte. Decima's
suggestion of a lagoonal interval (op. cit., p. 86) is based on a single,
meagre assemblage constituted for the greater part of Ammonia beccarii var.
tepida and some Cyprideis fragments. This level was not found in nearby
outcrops. Magne et al. suggested that the boundary-interval represented a
condensed zone and that detailed sampling might solve the problem. In
our opinion this problem is artificial and indicates only that the entries of
G. crotonensis and G. crassula should not be used for biostratigraphic zonations.
According to the revision of the planktonic foraminiferal biozonation of
the Mediterranean Pliocene (Cita, 197 5b), the upper part of the Trubi is
assigned to the Sphaeroidinellopsis subdehiscens Interval-zone. The basal
part of the Narbone formation corresponds to the Globigerinoides elongatus
Interval-zone which is defined by Cita (197 5b) as the interval with the zonal
marker from the extinction horizon of the genus Sphaeroidinellopsis to the
decline of Globigerinoides obliquus extremus. This massive decrease in
abundance virtually coincides with the entry of Globorotalia inflata (op.
cit., p. 540). In our counts G. inflata starts in sample 38. The frequency
distribution of G. obliquus/G. extremus does not show a massive decrease
in abundance towards this level. On the contrary maximum values are reached
well above the level of the appearance of G. inflata (fig. 47). Evidently
we are dealing with different species concepts of G. inflata (pers. comm.

FREQUENCY D ISTR I BUTION
OF SOME SELECTED
!:.::~:~~; •
47
46
45
oAA:
43
·>~:2:.:.
41
::A:

Mrs. Cita), which causes our G. inflata to enter the section some 70 meters
below the appearance of the species ofCita (Cita and Decima, 1975, p. 219,
221).
Gartner (in Cita and Gartner, 1973) describes the appearance of Pseudoemiliana
lacunosa from sample ROS 38. In deep-sea sediments this taxon
appears in the lower part of the Gauss Normal Epoch at about 3.1 to 3.2
m.y. B.P. (op. cit., p. 546).
In fig. 6 of Ryan et al. (1974) the top of the Trubi formation is made to
coincide with the upper boundary of the Spongaster pentas Zone, with the
boundary between NN 15 and NN 16 and with the lowermost part of N 21.

BENTHONIC FORAMINIFERAL ASSOCIATIONS THROUGHOUT THE SOUTH SICILIAN
PLIOCENE
For an analysis of the overall changes of the benthonic foraminiferal assemblages
throughout the Trubi and Monte Narbone formations the sections
were divided into eight successive lithological units:
1) a basal Trubi unit comprising the lowermost 21 samples (1393-73),
2) the non-laminated beds (19 samples) which alternate with
3) the laminated beds (16 samples),
4) four samples from the middle part of the Trubi at Lido Rossello,
5) the Trubi top part at Punta Piccola (PP 1-7),
6) the grey marls of the Narbone formation which alternate with
7) the ferromangenese-rich interbeds,
8) four samples of the upper part of the Narbone formation, at Lido
Rossello.
For the laminated/non-laminated sediments of groups 2 and 3 a closer
set of samples was available which was used for the simultaneous, study
in the programme of the project "Accuracy in Time" (Brolsma, 1978,
V.M.B.17).
The benthonic faunas were split more or less arbitrarily into ten groups.
Fig. 48 shows the species involved in this grouping. The groups are:
1) epiphytes sensu stricto, comprising only those taxa whose adhering
mode of life is known from the literature,
2) possible epiphytes, which incorporate species suspected of a sessile
and adhering mode of life,
3) mud-dwellers, a group of forms which is incomplete since not all
mud-dwellers present are incorporated in this group; for other reasons
they were included in one of the following groups,
4) Trubi-runners, a group in which typical Trubi species are assembled. In
this group Oolina hexagona is singled out as a separate subgroup, whereas
some other well-known or suspected mud-dwellers are also present
(Pleurostomella alternans, Gyroidina species, Siphonina bradyana,
Melonis barleeanus),
5) uniserials, another group of mud-dwelling species differentiated by
their chamber arrangement,

6) Uvigerina peregrina-pygmea and Hopkinsina bononiensis were grouped
for supposed ecological similarities,
7) Uvigerina proboscidea was regarded as a single group for its supposedly
high numbers in the laminated sediments,
8) Bolivina and Bulimina species taken together because of the posItIve
correlations shown by some with the manganese-rich layers of the
Narbone formation,
9) all arenaceous forms were combined for supposed ecological similarities,
10) the last group comprises the miscellaneous and indeterminable forms.
In fig. 48 the percentage-occurrences of these groups are shown in relation
to the lithological subdivisions; the last column shows the total number
of specimens per lithologic unit.
1) The epiphytes s.s. are a minor constituent of the faunas of the lower
part of the Trubi and do not show any preference for laminated or
non-laminated sediments. In the middle part of the Trubi this group
starts to increase in abundance and from the upper 10 ill of the Trubi
up to the top of the Narbone formation the group remains fairly
abundant between 17 and 23%. The manganese-rich intervals have the
lowest percentages (17%).
2) The percentages of epiphytes s.l. show a pattern distinctly different
from that of the epiphytes s.s. Serious doubt may be expressed about
their assumed mode of life. We probably included non-epiphytes in the
group. Percentages of around 10 occur throughout. However, in the
non-laminated beds within the laminated/non-laminated sequence, the
epiphytes s.l. are common, 18.5% versus 6% in the laminated beds. This
difference is mainly a consequence of the increased abundance of
Planulina ariminensis in this part of the section.
3) The mud-dwellers are fairly numerous (10 to 13%) throughout the
Trubi and Narbone formations. They are especially abundant in the
middle part of the Trubi (19%) and show sharply reduced percentages
in the laminated Trubi beds and manganese-rich intervals of the Narbone
formation (3.7 and 6.9% respectively).
4) The Trubi runners are dominant in the lower part of the Trubi (38 to
43%) and decrease towards the middle and top part of the Trubi and
in the overlying Narbone marls (13 to 16%). The group shows definitely
less affinity with the laminated sediments (14%) and more affinity
(43%) with the non-laminated beds.
The Golina hexagona subgroup occurs in low percentages (0.1 to 4%)

IK
<
.o~

throughout the Trubi and Narbone formations. It is strongly predominant
in the laminated Trubi sediments (48%). This high percentage is
reflected in the reduced percentage of most other groups with the
exception of Uvigerina proboscidea. These forms increase in number
despite the dominance of o. hexagona.
5) The uniserials, although rare throughout the sections (2 to 5%), are
slightly better represented in the laminated beds than in the nonlaminated
Trubi beds. Likewise they are twice as abundant in the
manganese-rich intervals as in the grey Monte Narbone marls. The
relative frequencies of this group are the opposite of those of muddwelling
group 3.
6) Uvigerina peregrina, U. pygmea and Hopkinsina bononiensis have relatively
few representatives throughout the sediments (0 to 8%); they
are rare to absent in the middle part of the Trubi without lithological
preference. This group seems to show a slight peak in the manganeserich
intervals of the Narbone formation (7%).
7) Uvigerina proboscidea is rare throughout the sections (0.02 to 3.47%)
but with a maximum of 5.7% in the laminated sediments versus 1.4%
in the accompanying non-laminated beds. No preference is recorded
for the manganese-rich or marly intervals in the Narbone formation.
8) The combined species of Bolivina and Bulimina are present with few
representatives throughout (0.35 to 6.75%), somewhat increasing
towards the top of the Narbone formation. There is a high peak of
21% in the manganese-rich intervals.
9) The arenaceous forms are fairly common throughout the sections (9
to 12%), with slightly lower percentages in the laminated Trubi beds
and in the manganese-rich intervals (approximately 7%), of which
especially the first one is probably of no significance.
10) The remaining group forms 6 to 11% of the assemblages throughout
the sediments without significant trends or changes, with the exception
of 17% in the upper four samples of the Narbone formation, on account
of the dominating presence of Cassidulina laevigata var. carinata.
Samples 42 to 45 and 153 to 156 of the Trubi and Narbone formations,
respectively, do not show major deviations from the overall picture. The
peak occurrence of mud-dwellers (19%) in the middle part of the Trubi is
balanced by the absence of other mud-dwelling forms such as U. peregrina,
U. pygmea and H. bononiensis.
Summarizing we conclude that there is a decreasing trend of typical Trubi
species throughout the Trubi-Narbone sequence. This decrease is compensat-

ed by the increase of epiphytes and the Bolivina-Bulimina group, which may
reflect a shallowing tendency and a greater supply of clay. Towards the
top the faunal composition starts to resemble that of the top-Miocene
Arenazzolo underneath. Superimposed on the general trends the laminated
beds and the manganese-rich beds show deviations in faunal association that
are clearly related to peculiar, though different, bottom conditions.
ARENAZZOLO
After the repeated eVapOrItIc phases of the Messinian had terminated,
the sands, silts and clays of the Arenazzolo were deposited in a shallow
marine environment with occasional brackish and even fresh water influences.
In addition to relatively small numbers of specimens re-worked from
older strata, the sediments contain indigenous and semi-indigenous foraminiferal
faunas which support the shallow water interpretation that is
indicated by the sedimentary features (cf. Brolsma, 1975b). Waves and
burrowing organisms were active intermittently, and sedimentation rates
were variable. The supply of sand decreased in an upward direction, and
ultimately only clay was slowly deposited, under quiet, low-energy conditions.
The calcium-carbonate content of the clay began- to increase and the
blue or green clays are seen to change gradually into marly clay, clayey
marl and marly limestone, and ultimately into hard and cream coloured
Turbi limestone. This change in lithology took place at such a slow pace
that burrowing organisms continued to criss-cross the sediments, their
holes being filled with material of contrasting colour from the overlying
and underlying sediments. The decreasing supply of fine terrigenous clastics
finally resulted in the slow accumulation of the purely biogenic limestone
of the Trubi.
Sedimentation conditions across the ill-defined boundary between Arenazzolo
and Trubi remained basically the same, i.e. slow accumulation under
low-energy conditions during the deposition of the Transitional interval.
There are no lithological data in the area to support the hypothesis of a
sudden, catastrophically increase in water-depth. The water-depth must have
increased fairly gradually. A steady ingression of the sea across a land of low
relief, which for a long time had supplied rather fine sediments, placed our
sections in a more offshore position, thus automatically cutting the supply
of suspended fines to the much smaller quantities of about 30% found in
the Trubi (op. cit., fig. 14).
This gradual change was occasionally interrupted locally by a renewed
supply of terrigenous clastics containing the typical Arenazzolo faunal

assemblages, after which the gradual change to biogenic sedimentation became
re-established. Such vertical alternations reflect rapid horizontal changes
in environmental conditions. They are of more regular occurrence in the
marginal areas of the Cattolica basin (Ogniben, 1957); they are strongly
reduced to scale or absent in the more central parts of the basin, i.e. in the
investigated successions on the southern coast of Sicily.
Paleobathymetrically the change from Arenazzolo to Trubi seems to
correspond to an increase in water-depth of only some 50 m. The maximum
depth of deposition for the cross-stratified Arenazzolo sediments has been
estimated at 50 m, and the lowermost Trubi faunas are indicative of depths
that are not necessarily in excess of 100 m (Brolsma, 1975b, p. 378).
The distribution and composition of the benthonic and planktonic assemblages
in the Arenazzolo and Transitional interval are in fair agreement with
the above assumptions. In the Arenazzolo we find faunal mixing of two
extreme benthonic assemblages, one preferring a muddy substrate and the
other living in shallow coastal waters rich in vegetation. Repeated: increase
of hydrodynamic forces in these shallow waters must have caused the
various mixtures of the faunas; ecological stress, probably caused by salinity
fluctuations, may be held responsible for their dwarfed nature. In the Transitional
interval and in the Trubi, preservation is better, and tests increase to
more normal dimensions. Faunal mixing decreases to a negligible degree.
The benthonic assemblages contain increasing numbers of species that prefer
muddy substrates but live today at depths exceeding 50 to 100 m. All true
shallow water forms disappear in the transitional strata and they are absent
in the overlying Trubi limestones.
The gradual faunal changes of benthonic and planktonic foraminifera
across the Transitional interval must be emphasized. The irregularities in
the distributional patterns of both the benthonic and the planktonic faunal
elements suggest unstable paleoecological conditions during sedimentation
of the transitional and lower Trubi sediments. Such vertical and horizontal
heterogeneity of the faunal distribution reflects the earlier recognized instability
of the water-masses and bottom conditions (Cita, 1973), but this
seems incompatible with faunal patterns in oceanic sediments of abyssal
depths. Another point worth mentioning is that all planktonic species
common in the Trubi are already present in comparable proportions in the
underlying Arenazzolo. Evidently sterilization of this part of the Mediterranean
at the end of the Messinian (Cita, 197 Sa) and the introduction of an
entirely new Atlantic fauna at the beginning of the Pliocene did not take
place.
The presence in substantial numbers of both Globorotalia margaritae and

G. puncticulata, recorded from Arenazzolo sediments down to some 12 m
below the Miocene-pliocene boundary (Brolsma, 197 Sa), is indicative of the
Mediterranean's earlier connections with the Atlantic Ocean in which the
former species is known to have evolved in Late Miocene times (see e.g.,
Parker, 1967, 1973; Blow, 1969; Berggren, 1973 and Brolsma, 1975a).
The introduction of G. puneticulata at this supposedly early date is more
problematic. It is possible, however, that the radiometric dating of its
evolutionary appearance is inaccurate, as suggested by Van Couvering et
al. (1976, p. 27 S), or that this evolutionary entry is just another diachronous
event. More favourable ecological factors are thought to have resulted in
the expansion, well above the base of the Trubi, of this taxon whose sudden
increase in numbers is commonly recognized in the literature as the species'
appearance level that is of biostratigraphic importance.
A gradual rise of sea-level and a slow rate of subsidence of the bottom
seem to be the mechanisms which eventually resulted in the ingression of the
sea, cutting short the supply of terrigenous material and causing a biogenic
sedimentation at relatively shallow depth. Indications of differential rates
of basin floor subsidence are found in the lower part of the Trubi in which
large scale slumping is observed, for instance at Eraclea Minoa (Brolsma,
1975b) and in the Pasquasia section.
Depositional rates were primarily determined by production of planktonic
biomass (Zachariasse, 1978), but a variable supply of terrigenous clastic fines
is thought to have played a role as well. The occasional more clayey intercalations
as well as the marly intervals seem to imply increased rates of sedimentation,
whereas lower rates are assumed for the homogenized and vaguely
bedded limestone beds as well as for the indurated intervals of the
short sequences described from the lower part of the section.
Acceleration of the production of the planktonic biomass seems to have
been responsible for the presence of the six laminated intervals. It has
become apparent that green algae, radiolarians, planktonic foraminifera and
diatoms increased considerably in numbers, thereby increasing the rate of
sedimentation to at least four times the rate calculated for the homogenized
and vaguely bedded limestones. Decomposition of the increased quantities of
organic material may have created adverse reducing conditions for bottom
life, especially below the sediment-water interface. Oxygen depletion at and
below the sediment-water interface was the result, enhancing the in situ formation
of pyrite in lamellae, as single grains and in bore holes, and obstruc-

ting oxygen-dependent bottom life. This process seems to have been responsible
for the preservation of the laminated beds and it explains the dwarfed
nature and the relatively smaller diversity of the surviving benthonic faunas
in these intervals.
Reducing conditions near the bottom, caused by decomposition of the
increased amounts of organic material, may be expected to cause notably
lower PH values as well. Since the remaining, though dwarfed, benthonic
foraminifera continue to be the calcareous ones, and arenaceous species
do not increase in relative numbers, it must be assumed that the unfavourable
PH effect was counterbalanced by the overwhelming quantity of carbonates
raining down as skeleton material of, especially, nannofossils and
foraminifera. If one assumes for the laminated intervals that the PH could
not affect the sediments because of the excess supply of carbonates, it
seems unlikely that a lowering of PH values can explain the hardgroundlike
top of so many small sequences lower down in the Trubi section. One
could suppose that the planktonic rains differed in composition. If there
were for some reason periodical peaks of organic planktonics and lows of
carbonate-secreting organisms, one might expect PH effects to result in
hardgrounds. The benthonic assemblages do not support this hypothesis;
nothing peculiar seems to happen in these sequences. On the other hand we
do know that blooms of siliceous organisms coincided with the deposition
of some of the laminated intervals, whereas for unknown reasons they are
conspicuously absent in others (U.M.B. 17).
The excessively high P/B ratios throughout the Trubi, which invoked ideas
of oceanic conditions and abyssal depths (Cita, 1973), must have been caused
by an abundant nutrient supply to the upper parts of the water masses.
Although it cannot be denied with certainty that supply from land-areas
played a role, the low percentages of clay admixture make such a major
source area for nutrients rather unlikely. If one accepts that a thermocline
was present during the later part of the Trubi sedimentation - post-Sphaeroidinellopsis
acme (Cita, 1976) - we cannot expect very strong effects from
an annual turnover in a subtropical region either. This leaves us with the
possibility that there was large scale upwelling, possibly caused by prevailing
eastward currents of Atlantic water through a connection wider than the
straits of Gibraltar today, across some open Balearic basin, and forced upward
by an incipient Italian rise or some Balkan-Greek mainland. It must be
borne in mind that the very high P/B ratios may also partly be caused by
the poverty of bottom faunas. It is possible that the low supply of terrigenous
material had an adverse effect on the bottom life. In this respect
it is worth mentioning that the most clayey intercalation represented in

our sample 93 suddenly shows a B/P rise to over 0.1, well above the usual
0.01-0.025 values. If the low clay supply can account for the high P/B
ratio of the regular Trubi, stronger upwelling on occasions could have been
another factor that explains the features of the laminated intervals.
The influence of shallower areas is occasionally shown by the presence
of plant remains and Chama-specimens from levels in the fifth laminated
interval and by a sudden bloom of benthonic diatoms (Schrader and Gersonde,
U.M.B. 17) in the same fifth interval (sample CRP 37).
The paleobathymerical reconstruction on the basis of the benthonic
foraminifera is hampered by the lack of characteristic species with narrow
upper and lower depth boundaries in the present oceans. A rather uniform
depth estimate between 100 and 926 m was obtained for the entire Trubi.
The presence of Nuttallides rugosus var. convexus might narrow this range
to 550 to 926 m if our only reference to this species is to be trusted as being
representative. Moreover, the lower depth boundary may be raised to 823 m on
account of the predominance of Nodosaria vertebralis var. albatrossi in two
of the samples. The most likely depth range thus established is only 273m
(from 550 to 823 m) but would be valid only for the laminated intervals.
However, the paleobathymetrical reconstruction is so uniform throughout
that rapidly changing depths of deposition can safely be excluded. It is
therefore reasonable to assume that the narrower depth range from about
500 to 800 m may be valid for the major part of the Trubi at Capo Rosselo.
From the observations on the Trubi intercalation in the Arenazzolo at
Eraclea Minoa and from the paleobathymetrical estimate for the sample
from Buccheri at the northern margin of the Ragusa platform, it may have
become evident that no identical paleobathymetrical reconstruction for
the Trubi at all these localities can be defended. The depth range estimated
for one locality may not overlap at all with the depth ranges concluded for
other localities. Along basinal margins such as those near Buccheri, Trubi
sediments were deposited at shallow depths ("v 200 m), and the same sedimentation
types extended down the slope (Capo Rossello) towards deeper
areas as, for instance, in the Southern Balearic Basin at site 371 (1100-
1400 m; see also Wright, 1977). From this pattern it follows that the paleobathymetry
at the various Trubi localities was a direct consequence of
some paleogeographic configuration existing already in Late Messinian
times. It is regarded as unlikely that the paleogeographic slopes towards
the basinal centres were formed only during deposition of the Trubi. One
would expect such a process to be reflected in the benthonic assemblages.
It is not surprising that no such indications of excessive Pliocene basinal
foundering have been found in the faunal succession in the core material

studied by Wright from site 371 (1977). Accentuation of slope and continued
foundering remain plausible, however.
A dip of the sea-floor in a SE direction at Capo Rossello is indicated by
the lateral movement of the loadcasts at the base of the first laminated
interval. The wavy stretches and fold structures at the base of the third
interval also point to an incline of the sea-floor and to occasional triggereffects
possibly caused by seismic activity.
Indications of differential rates of basin floor subsidence are also found
in the lower part of the Trubi at Eraclea Minoa (fig. 2, section 1). Large
scale slumping in S-SE direction has been observed (Brolsma, 1975b, pI. 3).
At the same locality, a few hundred meters SW of section 3 (see figs. 2, 49
and 50) the uppermost evaporitic beds of the Messinian are intensely folded
in larger, as well as in superimposed, smaller, folds. The axial planes dip in
a W-SW direction indicating that the direction of the movement of the over~
lying masses was towards the E-NE. These structures seem to be filled up
by Arenazzolo sediments which are in turn conformably overlain by the
Trubi limestones. The Arenazzolo attains a thickness of only 6 m instead of
16 m in section 1, which seems to indicate a loss of 10 m of sediment. This
Fig. 49 Southern tip of Capo Bianco, Eraclea Minoa, showing folded selenitic gypsum beds and the
overlying Arenazzolo and Trubi.

loss may be due to the folding. The intensity of the folding indicates that
these structures were formed under a considerable overburden of Trubi
sediments, if not of the entire unit. The Trubi mass seems to have slid downwards,
and the upper evaporitic beds and associated clays acted as lubricating

layers. This movement must have been over a short distance only since no
slip planes were observed and the Trubi-Arenazzolo contact seems to be
undisturbed. The exact time of this sliding cannot be ascertained.
The incline of sea-floor during deposition of the Trubi in a NE to SE
direction is indicated at both localities, at Eraclea Minoa and Capo Rossello.
This possibly points to a fairly consistent topography and the deeper centres
should therefore be sought in eastern or preferably in S-SE directions. This
basin-configuration may find support in the recent submarine topography
(cf. bathymetric chart in: The Mediterranean Sea, Stanley (ed.), 1972), in
which a NW-SE trending trough (down to 1700 m depth) extends between
the islands Pantellaria in the Wand Malta in the E.
The benthonic foraminiferal assemblages recovered from the Narbone formation
indicate primarily a normal, open marine environment in which
marly-clayey sediments were quietly deposited. The depth at which this
process occurred is difficult to estimate since real depth-indicative taxa are
absent. The marly-clayey substrate evidently attracted increasing quantities
of mud-feeders such as the Bolivina-Bulimina group which, however, are
poor bathymetric indicators. The growing importance of epiphytes recorded
from bottom to top may possibly be related to an increasing supply from
coastal areas or to a development of submarine vegetation in the vicinity.
By means of the preferential depths of the most common species the
depth of deposition was estimated to have been between 100 and 400 m,
tending to shallow in an upward direction. The increasing quantities of
mollusc-remains in the younger strata, also recorded from the same interval
in a nearby section by Magne et al. (1972), support this hypothesis.
Compared to the paleobathymetric reconstruction of the Trubi the
Narbone formation seems to have been deposited in a shallower environment.
The more clayey character of the younger formation is thought to
have influenced the deviating composition of the benthonic assemblages and
as a consequence our paleobathymetric estimate may be too shallow. However,
other lines of evidence, such as the changes in lithology, support the
idea of shallowing and an approaching hinterland, which supplied the terrigenous
fines and organic material in increasing quantities.
The B/P ratio rapidly increased in the lower part of the Narbone formation
to 41 specimens per 200 counted planktonic individuals, which either
indicates improving bottom conditions or decreasing plankton production.
The still higher B/P ratios, up to a maximum of 48, in the upper four samples
at Capo Rossello (section 6), would be in agreement with the inferred

shallowing tendency.
This quiet sedimentary process was interrupted at least 14 times by the
deposition of ferromanganese-oxides. Brines, which possibly originated from
subsurface volcanic activity in the area, were rapidly supplied and even
percolated through the topmost sediment. The impact of such brines on the
seawater chemistry is recorded in an area of at least a few km 2 • The effect
on the foraminiferal communities is visible in both the benthonic and the
planktonic assemblages.
Peaks in the B/P ratio coincide with these darker levels, suggesting that
either the productivity of benthonic foraminifera increased or that planktonic
life was suffering. The latter assumption is not substantiated by a
decrease in the number of planktonic species.
The species diversity of the benthonic foraminifera did decrease notably
in the manganese-rich layers. Most minimum values of the Fisher Cl'-index
correspond to these horizons. In many cases these low Cl'-indicesare caused
by the abundance of Bulimina aculeata, a species which may make up as
much as 50% of the assemblage. In the most strikingly dark interval this
species is entirely replaced by Bulimina exilis in an equally high percentage.
Epistominella smithi forms another abundant species in this interval G.
Higher in the section Bulimina inflata, Bolivina alata and Bolivina dilatata
also reach relative peaks in the manganese-rich intervals. Some of these
species (E. smithi, B. dilatata) are thought to increase in relative numbers
in low-oxygen environments (Harman, 1964). Similar faunas are found in
Lower Messinian deposits in the Mediterranean, in which near-euxinic
bottom conditions and increased salinity of the bottom waters are regarded
to have played a major role. Although the success of B. aculeata and the
other Bulimina and Bolivina species cannot be explained from known
environmental factors, it seems likely that the species-restricted benthonic
faunas consist mainly of elements that were capable of coping with the
worsened bottom conditions caused by activity of the pre-Etna.
The effect of the brines on the water chemistry of the overlying water
column seems to be demonstrated by the maximum percentages, up to
50%, of Globorotalia bononiensis in most of the darker horizons. It seems
likely that the same or related ecological factors simultaneously influenced
foraminiferal life at the bottom and in the overlying water column. The
distribution of the predominant species in both realms, B. aculeata and
G. bononiensis, is not identical. Deviations occur for instance in intervals
A, C, E and F from which B. aculeata is missing and in which G. bononiensis
is present. It appears that during deposition of interval C only planktonic
life was affected by the chemical changes, whereas no faunal anomalies were
recorded at the bottom. Only in the next higher interval D did the benthonic

fauna experience this change in environmental conditions. The effect of the
metalliferous solutions seems to have been more instantaneous for planktonic
life in the overlying water column than for the benthonic life at the
bottom. Although it seems plausible to hold the addition of metalliferous
solutions responsible for the changes in the water column, the effects were
different for both communities, and they also varied from interval to interval,
possibly as a result of variable conc~ntrations and durations of the chemical
admixtures.
Superimposed on this process decreasing water-temperatures are concluded
from the level of sample 33 upwards. The sudden bloom of Globigerina
bulloides in sample 35, the subsequent entry of Globorotalia inflata in
sample 38, and the tendency of Globigerina quinqueloba to increase in
numbers upwards, all point in this direction. The corresponding decrease in
numbers of the Globigerinoides group further supports this assumption. The
appearance of Globigerina pachyderma-types at the level of sample 43, again
corroborates the assumption of a cooling trend. Magne et al. (1972) arrived
at similar conclusions on the basis of malacofaunas which they recorded
from the nearby Realmonte section in strata corresponding to those of our
section 6.
The entry of Globorotalia inflata at the onset of cooler conditions seems
to be another, (now) demonstrable, example of an ecology controlled appearance
level, as was suggested before for the Globorotalia puncticulataentry.
The increased rate of clay deposition in the Punta Piccola section started
to obstruct burrowing life from the level of PP 35 upwards, as may be
inferred from the decreasing homogenization and the increasing number of
pyritic intervals.
It is generally accepted that there was a gradual change from biogenic to
more clastic sedimentation in the Middle Pliocene across the island of Sicily.
Middle to Upper Pliocene and even Lower Pleistocene sediments are deposited
in such clastic facies, spanning a considerable time interval. In combination
with the consistently decreasing depth of deposition up into the zone of
wave turbulence, it seems most appropriate to infer that a rising hinterland
was responsible for the ample supply of terrigenous clastic fines. Sea-level
oscillations undoubtedly were superimposed.
The absence of coarse terrigenous material throughout the entire length
of the Narbone section is believed to result from a lack of highly elevated
areas in the hinterland. Probably older sediments of small grain size or high
solubility (argille scagliose, turbidites, Tortonian marls and evaporitic sediments)
were the first to be eroded. If coarser detritus had been available
it would not have come further than the most marginal areas of the basin.

One of the major aims of this investigation was to get a better insight into
the local paleogeography at the end of the Miocene; this in its turn might
contribute to more general conclusions for the entire Mediterranean.
In the sections of Capo Rossello and Eraclea Minoa no clear evidence
was found for a desiccation phase during the deposition of the upper part
of the evaporation cycles. Characteristic desiccasion features such as shrinkage-cracks
or emersion levels have not been observed. A continuous water
cover must have remained. Water-depth cannot be reconstructed with certainty,
but it is thought to have been less than 100 meters. A similar depth
can be concluded for the overlying Arenazzolo.
The gradual lithological change from clastics to carbonates, which is
demonstrated by the Transitional interval between Arenazzolo and Trubi
(fig. 5) and by the occasional alternation of Trubi with typical Arenazzolo
faunas (section 3, Eraclea Minoa, chapter III) is merely a reflection of a
horizontal facies shift in the course of a relatively short time. This resulted
in greater water-depths in the investigated area of the Cattolica basin in an
early phase of the Trubi deposition.
The faunal changes across the boundary interval and within the lower part
of the Trubi reflect the increasing influence of Atlantic waters, which do not
seem to have advanced so catastrophically as proposed by Hsu, Cita and
Ryan (1973). The invading Atlantic waters obviously progressed across a
shallow sea, and drowned an adjoining land area of low relief. The paleogeographical
position of each locality determined the resulting succession of
strata. The reason that such influences are not found in basinal centres of
the Mediterranean may be either the distance from a source of clastic inflow,
or the presence of landward-situated sediment traps.
The paleobathymetrical estimates of the Trubi at Buccheri, Capo Rossello
and site 371, reveal different depositional depths of this sediment-type
in the same relatively short biostratigraphic interval. For the corresponding
time interval in the Early Pliocene a sea-floor gradient can be reconstructed
from the margin of the Cattolica basin to the more interior parts of the
Balearic basin; this gradient goes from roughly 50 meters to around 1400
meters over a distance of some 700 km, corresponding with a sea-floor
gradient of only 7 minutes. Of course it is realized that such a gradient is
only hypothetical and that there were probably many deeps and shallows

etween site 371 and Sicily.
These observations and conclusions together lead to the probability of
a multi-depressional paleogeography for the entire Mediterranean during
at least Late Miocene/Early Pliocene times. This multi-depressional Mediterranean
model was proposed by Marks (in Drooger, 1973) in an effort to
explain the seemingly conflicting implications of the two contradictory
models. The model envisages a checkered pattern which was tectonically
determined and consisted of many sub-basins of variable depths separated
by various structural highs. Such partitioning of basins into sub-basins by
differential tectonics is a widely recognized phenomenon in land areas such
as Spain, Northern Italy, Calabria (Roda, 1967) and the Aegean region
(Meulenkamp, 1977), during Messinian and Early Pliocene times. Each
sub-basin shows its particular succession of strata across the Miocene-pliocene
boundary even over small lateral distances, as described from Calabria
(Roda, 1967) and Crete (Meulenkamp et al., 1977). It seems justified to
assume that such processes are valid for a greater part of the Mediterranean.
Soon after the Early Pliocene transgression, the fault systems delineating the
various sub-basins became reactivated, which resulted in rapid subsidence
of these sub-basins. The rate of subsidence, however, may have varied from
basin to basin, being moderate along intermediate and marginal areas and
more rapid in central areas (Drooger, 1973, p. 271). This might have resulted
also in the different paleobathymetrical depth estimates obtained for the
Trubi in these central areas. If one considers the thickness distribution of
the evaporites such differential subsidence was equally valid for the Messinian
and possibly for somewhat older times. After a period of time these
subsidence rates were stabilized, keeping pace with the rate of accumulation,
as was observed in the middle and upper parts of the Trubi at Capo Rossello.
This section shows a seemingly uniform bathymetric record from the middle
part upwards, which seems to imply the relative stability of the slope or a
slight subsiding tendency balancing the sediment accumulation. In contrast
to the "desiccated, deep basin model" of Hsu, Cita and Ryan (1973), this
alternative model involves syn- and post-Messinian subsidence and may easily
account for the apparent paradox of Trubi in deep basinal settings and
elevated land sections. The sections on the Sicilian south coast seem to have
been located in an intermediate paleogeographical realm, i.e. on the slope
from shoals to deeps (Draoger, 1973, p. 268).
The abyssal depth suggestion for all Trubi sediments, concluded from the
extremely high P/B ratios, can be explained by an overwhelmingly rich
planktonic life, caused by ample inflow of nutrient-rich Atlantic waters and
more or less continuous upwelling phenomena. The Early Pliocene Mediter-

anean evidently had a nutrient supply that was completely different from
the self-supporting pattern of today because of the negligible inflow capacity
of the narrow Gibraltar Strait.
The combined presence of Globorotalia margaritae and G. puncticulata in
the Arenazzolo and their belated blooms in the overlying Trubi - generally
recognized as their subsequent true appearance levels - indicate that the
introduction of Atlantic waters across the shallow or narrow (Gibraltar?)
portal became amplified already after the ultimate evaporitic cycle. The lack
of major erosional surfaces or total desiccation levels in the upper evaporites
at Eraclea Minoa and Capo Rossello points to a constant water and/or brine
cover as a consequence of constant, though probably more restricted inflow
during the Late Messinian as well. The final, unimpeded influx of Atlantic
waters which started Trubi sedimentation, seems to have resulted in a sealevel
rise of only a few hundred meters in the marginal and slope areas
represented by the sections of Buccheri and Capo Rossello. The increasing
depth of deposition in the lower part of the Trubi is evidenced by the
benthonic faunal distribution of the Trubi intercalation in the topmost
Arenazzolo at Eraclea Minoa (section 3, estimated depth about 100 m)
and in the lowermost few meters of the Trubi at Capo Rossello. Here the
maximum depth of deposition increased to between 500 and 800 m, while
the addition of allochthonous shallow water forms sharply decreased. This
depth of deposition, once attained, seems to have remained quite uniform
for a measure of time, only to decrease again when the more clastic sedimentation
was resumed in the Narbone formation.
In basinal centres the relatively rapid rise in Early Pliocene sea-level might
give the impression that there had been a "catastrophic event", since the
depositional depth quickly increased to between 1100 and 1400 m (Wright,
1977). An extrapolation of this catastrophic event to the entire Mediterranean
does not seem justified in view of our data from Sicily. Unfortunately,
the depth at which the equivalents of the Arenazzolo were deposited at
these central sites is unknown due to the poor core-recovery of these unconsolidated
sediments.
The presence of indigenous planktonics in the Arenazzolo and between
the evaporites of the Messinian may be explained by a water stratification
with an upper layer of fresh Atlantic inflow of fairly normal sal~nity, floating
with its planktonic faunas on denser, more saline waters in the deeper parts of
the basins. Such a layering is conceivable if the Gibraltar area was in continuous
open connection with the Atlantic; there must have been some kind of Alboran
sluice with bordering shoals behind it, in which the water level was
close to Atlantic sea level (Drooger, 1973, p. 269). This hypothesis seems to

find support in the description of Messinian, open marine deposits at site
121 (D.SD.P., leg 13) in the Alboran Sea, as recorded by Montenat and
Bizon (1975). Originally, the absence of evaporites led Ryan et al. (1973)
to conclude that there was a hiatus between Tortonian and Lower Pliocene
marls. These new results, however, indicate an open connection with the
Atlantic during the Messinian or for at least part of it.
The results of this investigation seem to harmonize, to a certain extent,
the two conflicting models and to give strong support to the multi-depressional
model. Generalizations about the Trubi's depositional environment
have proved to be misleading. The newly proposed depositional mechanisms
need further testing, and more information about the Trubi near basin margins
may yield further clarifications.

A taxonomical treatment of all figured or discussed species of benthonic
and planktonic foraminifera was considered unnecessary. Only those taxa
on which some remarks were needed are included in this chapter. All types
are catalogued and deposited in the department of Stratigraphy and Micropaleontology
of the Geological Institute of the State University of Utrecht.
Ammonia beccarii (Linnaeus)
PI. 3, figs. 6a-b
Nautilus beccarii Linnaeus, 1758, Syst. Nat., 10, 1: 710, pI. 1, figs. la-c.
Ammonia beccarii (Linnaeus), Broekman, 1974, Utrecht Micropal. Bull. 8: pI. 1, fig. 4.
Remarks: This form differs from the typical form through the absence of
pillars and bosses in the umbilicus. It somewhat resembles the tepida variety
(Cushman, 1926, PubI. Carnegie Inst. Washington, 344, pI. 1), but differs in
its less convex dorsal side.
cibicides bradyi (Trauth)
PI. 4, figs. la-2c
Truncatulina bradyi Trauth, 1918, Denkschr. K. Akad. Wiss. Wien, Math.-Nat. CI., 95: 235.
Cibicides bradyi (Trauth), Barker, 1960, Taxonomic Notes, pI. 95, fig. 5; Pflum and Frerichs, 1976,
Cushman Found. For. Res., Spec. Publ., 14, pI. 3, figs. 6, 7.
Remarks: Specimens incorporated in this group show a gradual transition
to Cibicides robertsonianus (Brady) (pI. 4, figs. 3a-c), a common species in
the Narbone formation. The bradyi types are small planoconvex forms
(pI. 4, figs. la-c) which grade into more biconvex and large forms with
more convolutions (pI. 4, figs. 2a-c). The typical robertsonianus types are
slightly evolute at the ventral side and less biconvex. A transition from
predominant bradyi to robertsonianus takes place in the lower part of the
Narbone formation (pI. 4, figs. la-3c). pflum and Frerichs (1976) recorded
a similar intergradation of the two species in recent material from the Gulf
of Mexico.

Epistominella exigua (Brady)
PI. 2, figs. 4a-c
Pulvinulina exigua Brady, 1884, Rept. Voy. Challenger, Zool., 9: 696, pI. 103, figs. 13, 14.
Epistominella exigua (Brady), Parker, 1954, Bull. Mus. Compo Zool., 111 (10), pI. 10, figs. 22, 23.
Remarks: In all samples a wide variation exists in the number of chambers
per whorl, from 4 to 7. According to Wright (1977) forms with 5-5~ chambers
per whorl would prefer depths greater than 450 m, forms with 6-6~
chambers would not extend beyond that depth. No preference for any
specific number of chambers per whorl was found in our material.
Gyroidina soldanii d'Orbigny
PI. 2, figs. 7a-8c
Gyroidina soldanii d'Orbigny, 1826, Ann. Sci. Nat., 7: 278, no. 36; Longinelli, 1956, Palaeontogr.
Ital., 49, pI. 14, figs. 16a, b.
Remarks: Morphologically deformed specimens repeatedly occur in the
Arenazzolo and transitional deposits (pI. 2, figs. 7a-b). These aberrant forms
do not seem to have undergone post-mortem changes in morphology but
seem to have suffered from unfavourable bottom conditions preventing
a normal test construction.
Siphonina bradyana Cushman
PI. 3, figs. 3a-b
Siphonina bradyana Cushman, 1927, U.S. Nat. Mus., Proc., 72 (20): 11, pI. 1, figs. 4a-c; 1931, U.S.
Nat. Mus., Bull., 104 (8), pI. 14, figs. 4a-c; Barker, 1960, Taxonomic Notes, pI. 96, fig. 8.
Remarks: The fragile, non-tubulate outer-half of the carina is mostly brokenoff
in our material. This species differs from Siphonina reticulata (Czjzek)
by the coarse perforations near the sutures at the ventral side; this feature
is not shown on any of the figured reticulata specimens in either Czjzek
(1848, Haidinger's Nat. Abhandl., 2, pI. 13, figs. 7-9) or more recent
literature.
Globigerina bulloides d'Orbigny
PI. 6, fig. 1
Globigerina bulloides d'Orbigny, 1826, Ann. Sci. Nat., 7: 277, no. 17,76; Tjalsma, 1971, Utrecht
Micropal. Bull. 4, pI. 10, figs. 4a-c; Zachariasse, 1975, Utrecht Micropal. Bull. 11, pI. 16, fig. 6.

Remarks: Globigerina pseudobesa (Salvatorini) is considered a morphotypic
variant and consequently incorporated in G. bulloides. Initially, however,
this variant was recognized as a separate entity and is shown as such in the
distribution charts. The marked increase in numbers of G. bulloides in the
upper half of the Punta Piccola section from the level of PP 35 upwards is
accompanied by a similar increase of G. pseudobesa which indicates the
close relationship between these two forms.
Clobigerina nepenthes Todd, 1957, U.S. Ceol. Survey, Prof. Paper, 280-H: 301, pI. 78, figs. 7a-b;
Tjalsma, 1971, Utrecht Micropal. Bull. 4, pI. 11, figs. 3a-b; Zachariasse, 1975, Utrecht Micropal.
Bull. 11, pI. 16, fig. 4.
Remarks: To speed up the counting procedure the representatives of G.
decoraperta and G. nepenthes were considered as one group since separation
of the two species is often difficult and appeared to be subject to changes in
appreciation in the course of the investigation.
Globigerina quinqueloba Natland
PI. 6, fig. 5
Clobigerina quinqueloba Natland, 1938, Scripps Inst. Oceanogr., Bull., tech. ser. 4: 149, pI. 6, figs.
7a-c; Asano, Ingle and Takayanagi, 1968, Proe. 4th Sess. CMNS, Bologna, 1967, Ciorn. Ceol.,
(2a), 35, (2): 217-246, figs. 4,6,8,9,11 and 12.
Turborotalita quinqueloba (Natland), Bizon and Bizon, 1972, Atlas prine. foram. plane. bass. Med.,
pI. 284, figs. 1-7.
Remarks: The representatives of G. multiloba and G. quinqueloba have been
considered as one group in the counting procedure.
Globigerinoides trilobus (Reuss)
PI. 6, fig. 8
Clobigerina triloba Reuss, 1850, Denksehr., K. Akad. Wiss. Wien, Math.-Nat. CI. 1: 374, pI. 47, figs.
11a-d.
Clobigerinoides trilobus (Reuss), Tjalsma, 1971, Utrecht Mieropal. Bull. 4, pI. 15, figs. 1a-b,2-3.
Remarks: Globigerinoides sacculiferus (Brady) (pI. 6, fig. 11) is considered
a morphotypic variant of G. trilobus, as discussed earlier by Zachariasse
(1975, p. 131). Initially the variant was counted as a separate entity and is
shown as such in the distribution charts.

Globorotalia bononiensis Dondi
PI. 7, figs. 3a-7f; pI. 8, figs. la-2f
Globorotalia bononiensis Dondi, 1963, Bol!. Soc. Ceo!. Ita!., 81: J 62, p!. 4, figs. 41-45; Zachariasse,
1975, Utrecht Micropa!. Bul!. 11, p!. 14, figs. la-c.
Remarks: In the upper part of the Punta Piccola section a morphological
gradation was observed between this species and Globorotalia inflata
(d'Orbigny) (pI. 8, figs. 3a-6f). This morphological transition takes place
across a 7-8 m thick interval from samples PP 36 to 47. The main morphological
changes are formed by:
1) the decrease in number of chambers per whorl from 4~-4 to 4-3~,
2) the decrease in height of the aperture,
3) the shape of the chambers which become increasingly less globose, and
4) the spiral whorl which becomes more compact; consequently the width
of the umbilicus decreases.
Gradstein (1974) described a similar transition between the two groups
from a single section (Francocastello II) in Crete (p. 95, pI. 7, figs. 1-8).
Uncertainty remained as to whether his single example of a transition was
accidental or not. Colalongo and Sartoni (1967) suggested a lineage from
G. bononiensis to G. inflata on the basis of material from the Po valley.
The presence of a similar trend in our material from Southern Sicily seems
to point to an all-Mediterranean significance of this transition.
Globorotalia
margaritae Bolli and Bermudez
PI. 6, figs. 9-10
Globorotalia margaritae Bolli and Bermudez, 1965, Boll Inf. Venez. Ceo!. Min. Petr., 8: 139, p!. 1,
figs. 16-18; Zachariasse, 1975, Utrecht Micropal. Bul!. 11, pl. 13, figs. 4a-6c.
Remarks: The laminated deposits in the Trubi tend to contain a greater
number of thin-shelled and usually keeled forms (pI. 6, fig. 10), whereas
non-keeled, thick-shelled forms (pI. 6, fig. 9), seem to be more numerous
in the non-laminated Trubi intervals.
Globorotalia puncticulata (Deshayes)
PI. 7, figs. la-2d
Globigerina puncticulata Deshayes, 1832, Encyclopedie Methodique; Hist. Nat. de Vers, Mme. v.
Agasse, 2 (2): 170.
Globorotalia puncticulata (Deshayes), Banner and Blow, 1970, Cushman Found. For. Res., Contr.,
11, p!. 5, fig. 7 (lectotype).
Globorotalia puncticulata group, Cradstein, 1974, Utrecht Micropal. Bull. 7, pl. 5, figs. 1-6; pl. 6,
figs. 5-10.
Globorotalia puncticulata (Deshayes), Zachariasse, 1975, Utrecht Micropal. Bull. 11, pl. 14, figs. 2a-c.

Remarks: Colalongo and Sartoni (1967) suggested a phylogenetic transition
from G. puncticulata to G. bononiensis. Gradstein (1974) rejected this
suggestion of morphological transition on the basis of a statistical analysis
of quantitative data obtained from material from North Italian, West Sicilian
and Cretan sections.
Although not enough material is available, the assemblages from successive
samples from the Punta Piccola section (PP 4, 6, 11 and 20) seem to be in
favour of an intergradation of G. puncticulata to G. bononiensis. The chambers
become increasingly more inflated and the aperture tends to increase in
size, becoming highly arched. The periphery changes from slightly rounded
to broadly rounded. However, we did not find a continuous documentation
for the change in our section.
Neogloboquadrina acostaensis (Blow)
PI. 6, fig. 15
Globorotalia acostaensis Blow, 1959, Bull. Amer. Pal., 39 (178): 208, pI. 17, figs. 106a-c.
Globigerina globorotaloidea Colom, Tjalsma, 1971, Utrecht Micropal. Bull. 4, pI. 8, figs. 8a-b; pI. 9,
figs. 1a-3.
Globigerina acostaensis (Blow), Zachariasse, 1975, Utrecht Micropal. Bull. 11, pI. 15, figs. 3a-4c.
Remarks: Close-coiled pachyderma-types are incorporated in the variation.
The number of pachyderma-types increases towards the top of the Narbone
formation.
Sphaeroidinellopsis
group
Remarks: The few representatives of this genus have been considered as one
group in the counting procedure. Specimens belonging to S. seminulina
(Koch) and S. subdehiscens (Blow) may be recognized (cf. Cita and Gartner,
1973, pI. 51, figs. 1,4 and 6, respectively).

NUMBERED LITERATURE REFERRING TO BATHYMETRIC
RANGE CHARTS
1. Parker, F. L. (1958). Eastern Mediterranean Foraminifera. Rep. Swedish Deep Sea Exped.,
1947 --1948, v. 8, pp. 219 ·-283, Gotenborgs Kung!. Vetenskap Vitterhets Samhalle.
2. Walton, W. R. (1955). Ecology of living benthonic foraminifera, Todos Santos Bay, Baja Calif.,
J. ofPa!., v. 29, n. 6, pp. 952-1018.
3. Lankford, R. R. and Phleger, F. B. (1973). Foraminifera from the nearshore turbulent zone,
western North America. J. of Foram. Res., v. 3, n. 3.
4. Bandy, O. L. and Arnal, R. E. (1957). Distribution of recent foraminifera off West Coast of
Central America. Bull. Am. Ass. PetL Geol., v. 41, n. 9, pp. 2037-2053.
5. Drooger, C. W. and Kaasschieter, J. P. H. (1958). Foraminifera of the Orinoco-Trinidad-Paria
Shelf. Rep. Orinoco Shelf Exped., Verh. Kon. Ned. Akad. Wet., afd. Natuurk., Ie serie, v. 22.
6. Seiglie, G. A. (1966). Distribution of foraminifera in the sediments of Araya-Los Testigos shelf
and upper slope. Carib. J. Sci., v. 6, n. 3-4, pp. 93-117.
9. Bandy, O. L. and Rodolfo, K. S. (1964). Distribution of foraminifera and sediments, Peru-
Chili trench area. Deep-Sea Res., v. 11, pp. 817-837.
10. Murray, J. W. (1971). An Atlas of British Recent foraminiferids. Heinemann Educational Books
Ltd., London.
11. Blanc-Vernet, L. (1969). Contribution a l'etude des Foraminiferes de Mediterranee. Relations
entre Ie microfauna et Ie sediment. Biocoenoses actuelles, thanathocoenoses pliocenes et quaternaires.
Rec. Trav. Stat. Marit. d'Endoume, v. 64.
12. Ruscelli, M. (1949). Foraminiferi de due saggi di fondo del Mare Ligure. Atti Accad. Ligure
Sci. Lett., v. 6, n. 1, pp. 1-31.
13. Phleger, F. B., Parker, F. L. and Peirson, J. F. (1953). North Atlantic foraminifera. Rep. Swedish
Deep Sea Exp., v. 7, n. 1.
14. Phleger, F. B. (1951). Ecology of Foraminifera N.W. Gulf of Mexico. Geo!. Soc. America, Mem.
46, n.L
15. Parker, F. L. (1954). Distribution of the foraminifera in the N.E. Gulf of Mexico. Bul!. Mus.
Compo Zool. at Harvard ColI., v. 111, n. 10.
18. Chierici, M. A., Busi, M. T. and Cita, M. B. (1962). Contribution a une etude ecologique des
foraminiferes dans la mer Adriatique. Rev. de Micropa!. V. 5, n. 2.
19. Murray, J. W. (1973). Distribution and Ecology of living foraminiferids. Heinemann Educational
Books Ltd., London.
20. Pujos, M. (1971). Repartition des biocoenoses de Foraminiferes benthiques sur Ie plateau continental
du Golfe de Gascogne a l'Ouest de l'embouchure de la Gironde. Rev. Esp. Micropal., v. 4,
n. 2, pp. 141-156.
22. Cita, M. B. and Chierici, M. A. (1962). Crociera talassografica adriatica 1955, V. Ricerche sui
foraminiferi contenuti in 18 carote prelevate suI fondo del Mare Adriatico. Arch. Oceanogr.
Limn. v. 12, n. 3, pp. 297-359.
23. Pujos-Lamy, A. (1971). Les foraminiferes benthiques abyssaux: leur utilisation pour la mise en
evidence des variations climatiques dans une carotte du Quaternaire recent. C.R. Acad. Sc. Paris,
V. 272,pp. 215-218.
24. Pujos, M. (1970). Influence des eaux de type mediterraneen sur la repartition de certains foraminiferes
benthiques dans Ie Golfe de Gascogne. Cah. Oceanogr., v. 22, n. 8, pp. 827-831.
27. Phleger, F. B. and Parker, F. L. (1951). Ecology of Foraminifera, northwest Gulf of Mexico.
Geo!. Soc. America, Mem. 46, n. II.
28. Bock, W. D., Hay, W. W., Jones, J. L, Lynts, G. W., Smith, S. L. and Wright, R. C. (1971). A
symposium of recent South Florida foraminifera. Miami Geo!. Soc., Mem. L
29. Heron-Allen, E. and Earland, A. (1932). Foraminifera, Part L The icefree area of the Falkland
Island and adjacent seas. Discovery Reports, V. 4, pp. 291-460.

30. Earland, A. (1934). Foraminifera, Part III. The Falkland Sector of the Antarctic (excluding
South Georgia). Discovery Reports, v. 10, pp. 1-208.
31. Brasier, H. D. (1975). The ecology and distribution of recent foraminifera from the reefs and
shoals around Barbuda, West Indies.J. Foram. Res., v. 5, n. 3, pp. 193-210.
32. Zalesny, E. R. (1959). Foraminiferal ecology of Santa Monica Bay, California. Micropal., v. 5,
n. 1, pp. 101-126.
33. LeRoy, D. O. and Levinson, S. A. (1974). A deep-water Pleistocene microfossil assemblage
from a well in the northern Gulf of Mexico. Micropal., v. 20, n. 1, pp. 1-37.
34. Bandy, O. L. and Chierici, M. A. (1966). Depth-temperature evaluation of selected California
and Mediterranean bathyal foraminifera. Marine Geol., v. 4, pp. 259-271.
36. Levy, A. (1971). Eaux saumatres et milieux margino-littoraux. Rev. Geograph. Phys. Geol.
dyn.,v. 13,n.3,pp. 269-278.
37. Dupeuble, P. A., Mathieu, R., Momeni, I., Poignant, A., Rosset-Moulinier, M., Rouvillois, A.
and Ubaldo, M. (1971). Recherches sur les F oraminiferes actuels des cotes fran,aises de la Manche
et de la Mer du Nord. Rev. de Micropal., v. 14, n. 5, pp. 83-95.
38. Dupeuble, P. A., Mathieu, R., Momeni, I., Poignant, A., Rosset-Moulinier, M., Rouvillois, A. and
Ubaldo, M. (1972). Travaux recents sur les Foraminiferes actuels des cotes fran,aises de la
Manche. Mem. B.R.G.M., v. 79, pp. 97-100.
39. Mathieu, R. (1971). Les associations de Foraminiferes de plateau continental Atlantique du
Maroc au large de Casablanca. Rev. de Micropal., v. 14, n. 1, pp. 55-61.
40. Bandy, O. L. (1960). General correlation of foraminiferal structure with environment. Rep.
Internat'l. Geol. Congress, 21 session, Norden, part 22, pp. 7-19.
43. Pareira, C. A. F. D. (1969). Recent foraminifera of southern Brazil, collected by hydrographic
vessel "Baependi". Iheringia, ZooI., v. 37, pp. 37-95.
44. Colom, G. (1950). Estudio de los Foraminiferos de muestras de fondo recogidas entre los Cabos
Juby y Bojador. Bol. Inst. Esp. Oceanogr., v. 28, pp. 1-45.
45. D'Onofrio, S. (1959). Foraminiferi di una carota sottomarina del medio Adriatico. Giorn. Geol.,
serie 2a, v. 27, pp. 147~190.
47. Pujos-Lamy, A. (1973). Repartition bathymetrique des foraminiferes benthiques profonds du
Golfe de Gascogne. Comparaison avec d'autres aires oceaniques. Rev. Esp. Micropal., v. 5, n. 2,
pp.213-234.
51. Bandy, O. L. (1961). Distribution of foraminifera, radiolaria and diatoms in sediments of the
Gulf of California. MicropaI., v. 7, n. 1, pp. 1-26.
52. Ph leger, F. B. (1964). Patterns of living benthonic foraminifera, Gulf of California. Am. Assoc.
Petr. Geol., Mem. 3, pp. 377-394.
53. Cushman,J. A. (1918). The foraminifera of the Atlantic Ocean. U.S. Nat. Mus., Bull. 104.
54. Brady, H. B. (1884). Report on the scientific results of the voyage ofH. M. S. Challenger.
Zoology, v. 9.
55. Iaccarino, S. (1967). Ricerche sui foraminiferi dell'alto Adriatico. Arch. Oceanogr. Limnol.,
v. 15, n. 1, pp. 11-54.
56. Iaccarino, S. (1967). Ricerche sui foraminiferi contenutti in sei carote prelevate nelMare Ligure
(La Spezia). Bol. Soc. Geol. It., v. 86, pp. 59-88.
57. Iaccarino, S. (1964). Ricerche preliminari sui foraminiferi contenu ti in 3 carote prelevate nel
Mare Ligure (La Spezia). BoI. Soc. GeoI. It., v. 83, n. 1.
58. Iaccarino, S. (1969). I foraminiferi di campioni di fondo prelevati nel Golfo di Taranto (M.
Ionio). "L'Ateneo Parmense"-Acta Naturalia, v. 5, n. 1.
61. Uchio, T. (1960). Benthonic foraminifera of the Antarctic Ocean. Spec. Publ., Seto Marine
BioI. Lab., BioI. Results of the Japanese Antarctic Res. Exp., v. 12.
62. Uchio, T. (1960). Ecology of living benthonic foraminifera from the San Diego, California,
area. Spec. Publ., Cushman Found. For. Res., no. 5.
65. Anderson, J. B. (1975). Ecology and distribution of foraminifera in the Weddell Sea of Antarctica.
Micropal., v. 21, n. 1, pp. 69-96.

67. Egger, J. G. (1893). Foraminiferen aus Meeresgrundproben, gelothet yon 1874 bis 1876 yon S. M.
Sch. Gazelle, Abh. K. Akad. Wiss., II Kl., 18 Bd., II Abth., Miinchen.
69. ]arke,]. (1960). Beitrag zur Kenntnis der Foraminiferen fauna der Mittleren und Westlichen
Barents-See. Int. Revue ges. Hydrobiol., v. 45, n. 4, pp. 581-654.
71. Le Calvez, Y. (1958). Les Foraminiferes de la Mer Celtique. Rev. Trav. Inst. Peches marit., v. 22,
n.2.
74. Le Calvez, Y. (1972). Etude ecologique de quelques foraminiferes de la cote saharienne de l'Atlantique.
Rev. Trav. Inst. Peches marit., v. 36, n. 3, pp. 245-254.
75. Caralp, M., Lamy, A. and Pujos, M. (1970). Contribution a la connaissance de la distribution
bathymetrique des foraminiferes dans Ie Golfe de Gascogne. Rev. Esp. Micropal., v. 2, n. 1, pp.
55-84.
76. Cushman,]. A. (1942). The foraminifera of the tropical Pacific, collections of the "Albatross",
1899-1900. U.S. Nat. Mus., Bull., v. 161, n. 3.
79. Barbieri, F. and Medioli, F. (1969). Distribution of foraminifera on the Scotian Shelf (Canada).
Riv. Ital. Paleont., v. 75, n. 4, pp. 849-878.
80. Bandy, O. L. (1953). Ecology and paleoecology of some Californian foraminifera. Part 1. The
frequency distribution of recent foraminifera off California. ]. ofPaleont., v. 27, n. 2.
81. Todd, R. and Low, D. (1966). Foraminifera from the Arctic Ocean off the Eastern Siberian
Coast. U.S. Geol. Survey, Prof. Paper, 550-C, pp. C79-85.
82. Wright, R. (1977). Neogene paleobathymetry of the Mediterranean based on benthonic Foraminifera
from D.S.D.P.leg. 42A. Init'l Rep. D.S.D.P., v. 42 (in press).
85. Voorthuysen,]. H. van (1973). Foraminiferal ecology of the Ria de Arosa, Galicia, Spain. Zool.
Verhandelingen, no. 123.
87. Frerichs, W. E. (1970). Distribution and ecology of benthonic foraminifera in the sediments of
the Andaman Sea. Contr. Cushman Found. For. Res., v. 21, n. 4, pp. 123-147.
88. Pflum, C. E. and Frerichs, W. E. (1976). Gulf of Mexico deep-water foraminifers. Spec. Publ.,
Cushman Found. For. Res., no. 14.

Anderson, G. ]. (1963). Distribution patterns of recent foraminifera of the Bering Sea. Micropal.,
v. 9,n. 3,pp.305-317.
Anderson,]. B. (1975). Ecology and distribution of foraminifera in the Weddell Sea of Antarctica.
Micropal., v. 21, n. 1, pp. 69-96.
Bandy, O. L. (1953). Ecology and paleoecology of some California Foraminifera. Part I. The frequency
distribution of recentForaminifera off California.]. of Paleont., v. 27, n. 2.
- (1961). Distribution of foraminifera, radiolaria and diatoms in sediments of the Gulf of California.
Micropal., v. 7, n. 1, pp. 1-26.
Barbieri, F. and Medioli, F. (1964). Significato paleoecologico di aleuni generi di foraminiferi nella
serie Pliocenica Vernasca-Castell'Arquato. "L'Ateneo Parmense", v. 35, n. 1, pp. 1-27.
- and - (1969). Distribution of foraminifera on the Scotian Shelf (Canada). Riv. Ital. Paleont., v. 75,
n. 4, pp. 849-878.
Be, A. W. H. and Tolderlund, D. S. (1971). Distribution and ecology of living planktonic foraminifera
in surface waters of the Atlantic and Indian Oceans. Micropal. of Oceans, Cambridge Univ. Press,
London.
Berger, W. H. (1970). Planktonic Foraminifera: Selective solution and the lysocline. Marine Geology,
v. 8, pp. 111-138.
Berggren, W. A. (1973). The Pliocene time scale: calibration of planktonic foraminiferal and calcareous
nannoplankton zones. Nature, v. 243, pp. 391-397.
Blanc-Vernet, L. (1969). Contribution a l'etude des foraminiferes de Mediterranee. Relations entre Ie
microfaune et Ie sediment. Biocoenoses actuelles, thanathocoenoses pliocenes et quarternaires.
Rec. Trav. Stat. Marit. d'Endoume, v. 64.
Blow, W. H. (1969). Late Middle Eocene to recent planktonic biostratigraphy. Proc. First Plankt.
Conf., Geneva 1967, pp. 199-241.
Boalch, G. T. and Parke, M. (1971). The Prasinophycean genera (Chlorophyta) possibly related to
fossil genera, in particular the genus Tasmanites. Proc. Second Plankt. Conf., Roma 1970, pp.
99-105.
Brady, H. B. (1884). Report on the scientific results of the voyage of H. M. S. Challenger. Zoology,
v.9.
Brasier, M. D. (1975). The ecology and distribution of recent foraminifera from the reefs and shoals
around Barbuda, West Indies.]. Foram. Res., v. 5, n. 3, pp. 193-210.
Brolsma, M. ]. (197 5a). Stratigraphical pro blems concerning the Miocene-Pliocene boundary in Sicily
(Italy). Proc. Kon. Ned. Akad. Wet., B, v. 78, n. 2, pp. 94-107.
(1975 b). Lithostratigraphy and foram iniferal assem blages of the Miocene-Pliocene transitional
strata of Capo Rossello and Eraclea Minoa (Sicily, Italy). Proc. Kon. Ned. Akad. Wet., B, v. 78,
n. 5, pp. 341-380.
- (1978). In: Zachariasse et aI., Micropaleontological counting methods and techniques - an exercise
on an eight metres section of the Lower Pliocene of Capo Rossello, Sicily. Utrecht Micropal.
Bull. 17.
Calvert, S. E. (1966). Accumulation of diatomaceous silica in the sediments of the Gulf of California.
Geol. Soc. Amer., Bull. v. 77, pp. 569-596.
Calvez, Y. Ie (1958). Les Foraminiferes de la Mer Celtique. Rev. Trav.lnst. Peches marit., v. 22, n. 2.
- (1972). Etude ecologique de quelques foraminiferes de la cote saharienne de l'Atlantique. Rev.
Trav. Inst. Peches marit., v. 36, n. 3, pp. 245-254.
Caralp, M., Lamy, A. and Pujos, M. (1970). Contribution a la connaissance de la distribution bathymetrique
des foraminiferes dans Ie Golfe de Gascogne. Rev. Esp. Micropal., v. 2, n. 1, pp. 55-84.
Ciaranfi, N. and Cita, M. B. (1973). Paleontological evidence of changes in the Pliocene climates.
Init'l Rep. D.S.D.P., v. 13, n. 2, pp. 13871399.
Cifelli, R. and Smith, R. K. (1974). Distributional patterns of planktonic Foraminifera in the western

North Atlantic. J. For. Res., v. 4, n. 3, pp. 112-125.
Cita, M. B. (1973). Mediterranean evaporite: paleontological arguments for a deep-basin desiccation
model. In: Messinian Events in the Mediterranean. Geodyn. Sci. Rep., v. 7, pp. 206-228.
(1975a). The Miocene-Pliocene Boundary. History and definition. In: "Symposium on Late Neogene
Epoch Boundaries". Intern. Geol. Congr., Montreal, 1972, Micropal. Press Spec. Publ., v. 1,
pp.1-30.
(1975b). Planktonic foraminiferal biozonation of the Mediterranean Pliocene deep sea record. A
revision. Riv. Ital. Paleont. Strat., v. 81, n. 4, pp. 527-544.
- (1976). Biodynamic effects of the Messinian salinity crisis on the evolution of planktonic foraminifera
in the Mediterranean. Paleogeogr., Paleoclim., Paleoecol., v. 20, pp. 23-42.
and Decima, A. (1975). Rossellian: proposal of a su perstage for the marine Pliocene. Proc. 6th
Congr. R.C.M.N.S. Bratislava, v. 1, pp. 217-227.
and Gartner, S. (1973). The stratotype Zanclean. Foraminiferal and nannofossil biostratigraphy.
Riv. Ital. Paleont. Strat., v. 79, n. 4, pp. 503-558.
Colalongo, M. L. and Sartoni, S. (1967). Globoro talia hirsuta aemiliana nuova sottospecie cronologica
del Pliocene in Italia. Giorn. Geol. Bologna, (2a), v. 34, n. 1, pp. 265-284.
Cuhman, J. A. (1918). The foraminifera of the Atlantic Ocean. U.S. Nat. Mus., Bull. 104.
Decima, A. (1964). Ostracodi del Gen. Cyprideis Jones del Neogene e del Quaternario italiani. Paleont.
Ital., v. 57, pp. 81-133.
Di Grande, A. (1969). L'alternanze neogenico-quaternaria di vulcaniti e di sedimenti al margine nordoccidentale
dell'Altipiano Ibleo. Atti Accad. Gioenia Sc. Nat. Catania, Serie 7, n. 1, pp. 91-125.
Di Napoli Alliata, E. (1964). Il Miocene superiore nella Valle dell'Orte presso Bologna (Pescara).
Geo!. Romana, v. 3, pp. 3-32.
Drooger, C. W. (1973). The Messinian Events in the Mediterranean. A Review. In: Messinian Events
in the Mediterranean. Geodyn. Sci. Rep., v. 7, pp. 263-272.
(1975). The Late Miocene Mediterranean. In: G. J. Borradaile, A. R. Ritsema, H. E. Rondeel and
O. J. Simon (editors), Progress in Geodynamics, Geodynamics Projects, Scientific Report, n. 13,
pp. 119-125. North-Holland Publishing Company, Amsterdam, New York.
- and Kaasschieter, J. P. H. (1958). Foraminifera on the Orinoco-Trinidad-Paria Shelf. Rep. Orinoco
Shelf Expcd., Verh. Kon. Ned. Akad. Wet., afd. Nat., 1e sede, n. 22.
Dupeuble, P. A., Mathieu, R., Momeni, I., Poignant, A., Rosset Moulinier, M., Rouvillois, A. and Ubaldo,
M. (1971). Recherches sur les Foraminiferes actuels des cotes fran~aises de la Manche et
de la Mer du Nord. Rev. de Micropal., v. 14, n. 5, pp. 83-95.
Egger, J. G. (1893). Foraminiferen aus Meeresgrundproben, gelothet von 1874 bis 1876 von S. M. Sch.
Gazelle. Abh. d.k. bayer. Akad. d. Wiss., II Kl., 18 Bd., II Abth., Munchen.
Emiliani, C. (1974). Isotopic paleotemperatures and shell morphology of Globigerinoides rubra in the
Mediterranean deep-sea core 189. Micropal., v. 20, n. 1, pp. 106-109.
Fisher, R. A., Corbett, A. S. and Williams, C. B. (1943). The relationship between the number of
species and the number of individuals in a random sample of an animal population. J. Anim.
Ecol.,v.12,pp.42-58.
Frerichs, W. E. (1970). Distribution and ecology of benthonic foraminifera in the sediments of the
Andaman Sea. Cushman Found. For. Res., Contr., v. 21, n. 4, pp. 123-147.
Gradstein, F. M. (1974). Mediterranean Pliocene Globorotalia. A biometrical approach. Utrecht Micropal.
Bull. 7.
Hantzschel, W. (1975). Treatise on Invertebrate Paleontology, Part W, Miscellanea, suppl. 1, Trace
fossils and Problematica, pp. 49-52.
Harman, R. A. (1964). Distribution of foraminifera in the Santa Barbara Basin, California. Micropal.,
v. 10,n. 1,pp. 81-96.
Hecht, A. D. and Savin, S. M. (1970). Oxygen-18 studies of recent planktonic Foraminifera: Comparisons
of phenotypes and of test parts. Science, v. 170, pp. 69-7l.
Heron-Allen, E. and Earland, A. (1932). Foraminifera, Part I, The ice-free area of the Falkland Islands
and adjacent seas. Discovery Reports, v. 4, pp. 291-460.

Hsii, K. J., Cita, M. B. and Ryan, W. B. F. (1973). The origin of the Mediterranean evaporites.1nit'l
Rep. D.S.D.P., v. 13, n. 2, pp. 1203-1231.
Iaccarino, S. (1964). Ricerche preliminari sui foraminiferi contenuti in 3 carote prelevate nel Mare
Ligure (La Spezia). Boll. Soc. Geol. Italiana, v. 83, n. 1.
- (1967). Ricerche sui foraminiferi dell'alto Adriatico. Arch. Oceanogr. Limnol., v. 15, n. 1, pp. 11-
54.
- (1969). I foraminiferi di campioni di fondo prelevati ne1 Golfo di Taranto (M. Ionico). "L'Ateneo
Parmense", Acta Naturalia, v. 5, n. 1.
J arke, J. (1960). Beitrag zur Kenntnis der Foraminiferenfauna der Mittleren und Westlichen Barents-
See. Int. Revue ges. Hydrobiol., v. 45, n. 4, pp. 581-654.
Kennedy, W. J. (1970). Trace fossils in the Chalk environment. In: Trace fossils, Crimes, T. P. and
J. C. Harper (eds), pp. 263-282.
Levy, A. (1971). Eaux saumatres et milieux margino-littoraux. Rev. Geograph. Phys. Geol. dyn., v. 13,
n. 3, pp. 269-278.
Magne, J., Mascle, G. et Mongin, D. (1972). Stratigraphie des formations du Miocene terminal au
Quarternaire en Sicile sud-occidentale. Bull. Soc. Geol. France, serie 7, n. 14, pp. 147-158.
Marchetti, M. P. (1957). The occurrence of slide and flowage materials (olistostromes) in the Tertiary
series of Sicily. Internat'l Geol. Congress Mexico 1956, 20th session, section 5, Relaciones
entre la tectonica y la sedimentacion, pp. 209-225.
- (1960). Summary introduction to geology of Sicily. Petro Expl. Soc. Lybia, pp. 47-60.
Mascle, G. (1974). Les grands traits de l'evolution geologique des Monts Sicani (Sicile). Bull. Soc.
Geol. France, serie 7, V. 16, pp. 161-170.
Mathieu, R. (1971). Les associations de Foraminiferes du plateau continental Atlantique du Maroc
au large de Casablanca. Rev. de Micropal., v. 14, n. 1, pp. 55-61.
Meulenkamp, J. E. (1977). The Aegean and the Mediterranean salinity crisis. Proc., 6th Coll. Geol.
Aegean Region, Athens 1977, (in press).
- Jonkers, H. A. and Spaak, P. (1977). Late Miocene to Early Pliocene development of Crete. Proc.,
6th ColI. Geol. Aegean Region, Athens 1977 (in press).
Montenat, Ch., Bizon, G. and J.-J. (1975). Remarques sur Ie Neogene du forage Joides 121 en Mer
d'Alboran (Mediterranee occidentale). Bull. Soc. Geol. France, serie 7, v. 17, n. 1, pp. 45-51.
Murray, J. W. (1973). Distribution and ecology of living benthic foraminiferids. Heinemann Educ.
Books Ltd., London.
Nesteroff, W. D. (1973). Mineralogy, petrography, distribution and origin of the Messinian Mediterranean
evaporites. Init'l Rep. D.S.D.P., v. 13, n. 2, pp. 673-694.
Ogniben, L. (1957). Petrografia della serie solfifera siciliana e considerazioni geologiche relative.
Mem. Descritt. Carta Geol. Ital., 33.
Pareira, C. A. F. D. (1969). Recent foraminifera of southern Brazil collected by hydrographic vessel
"Baependi", Iheringia. Zool., v. 37, pp. 37-95.
Parker, F. L. (1954). Distribution of the foraminifera in the N.E. Gulf of Mexico. Bull. Mus. Compo
Zool. at Harvard ColI., V. 111, n. 10.
(1958), Eastern Mediterranean Foraminifera. Rep. Swedish Deep Sea Exped., 1947-1948, v. 8,
pp. 219-283. Gotenborgs Kungl. Vetenskap Vitterhets Samhiille.
(1967). Late Tertiary biostratigraphy (planktonic foraminifera) of tropical Indo-Pacific deep-sea
cores. Bull. Amer. Paleont., v. 52, n. 235, pp. 115-203.
(1973). Late Cenozoic Biostratigraphic (planktonic foraminifera) of tropical Atlantic Deep-Sea
sections. Rev. Esp. Micropal., V. 5, pp. 253-289.
Phleger, F. B. (1951). Ecology of Foraminifera, N.W. Gulf of Mexico. Geol. Soc. Amer., Mem. 46.
- (1964). Foraminiferal ecology and marine geology. Mar. Geol., V. 1, pp. 16-43.
Pflum, C. E. and Frerichs, W. E. (1976) Gulf of Mexico Deep-Water foraminifers. Cushman Found.
For. Res., Spec. Publ. no. 14.
Pujos, M. (1970). Influence des eaux de type mediterraneen sur la repartition de certains foraminiferes
benthiques dans Ie Golfe de Gascogne. Cah. Oceanogr., v. 22, n. 8, pp. 827-831.

(1971). Repartition des biocoenoses de Foraminiferes benthiques sur Ie plateau continental du
Golfe de Gascogne a l'Ouest de I'embouchure de la Gironde. Rev. Esp. Micropal., v. 4, n. 3, pp.
141-156.
Radford, S. S. (1976). Recent Foraminifera from Tobago Island West Indies. Rev. Esp. Microp~l., v. 8,
n. 2, pp. 193-218.
Reiss, Z., Halicz, E. and Perelis, L. (1974). Planktonic Foraminiferida from recent sediments in the
Gulf of Elat. IsraeL]. Earth Sciences, v. 23, pp. 69-105.
Riedel, W. R. and Sanf:tlippo, A. (1978). In: Zachariasse et aI., Micropaleontological counting methods
and techniques - an exercise on an eight metres section of the Lower Pliocene of Capo Rossello,
Sicily. Utrecht Micropal. Bull. 17.
-, - and Cita, M. B. (1974). Radiolarians from the stratotype Zanc1ean (Lower Pliocene, Sicily). Riv.
Ital. Paleont. Strat., v. 80, n. 4, pp. 699-734.
Reineck, H. E. and Singh, I. B. (1971). Genesis of laminated sand and graded rhythmites in stormsand
of shelf mud. Sedimentology, v. 18, pp. 123-128.
Roda, C. (1967). I sedimenti neogenici autoctoni ed alloctoni delia zona di Ciro-Cariati (Catanzaro
e Cosenza). Mem. Soc. Geol. Ital, v. 6.
Ryan, W. B. F., Hsii, K. ]., Cita, M. B. Dumitrica, P., Lort, ]., Mayne, W., Nesteroff, W. D., Pautot, G.,
Stradner, H. and Wezel, F. C. (1973). Western Alboran Basin-site 121. Init'l Rep. D.S.D.P.,
leg 13, v. 1, pp. 43-91.
- Cita, M. B., Dreyfus Rawson, M., Burekle, L. H. and Saito, T. (1974). A paleomagnetic assignment
of Neogene stage boundaries and the development of isochronous datum planes between the
Mediterranean, the Pacific and Indian Oceans, in order to investigate the response of the world
ocean to the Mediterranean "salinity crisis". Riv. Ital. Paleont. Strat., v. 80, n. 4, pp. 631-688.
Salvatorini, G. (1968). I foraminiferi delle argille a Pycnodonta navicularis (Brocchi) del Miocene
superiore della Toscana Marittima. Soc. Toscana Sci. Natur., Atti, Mem., Ser. A, v. 75, n. 1, pp.
259-358.
Schrader, H. ]. and Gersonde, R. (1978). In: Zachariasse et aI., Micropaleontological counting methods
and techniques - an exercise on an eight metres section of the Lower Pliocene of Capo
Rossello, Sicily. Utrecht Micropal. Bull. 17.
Seilacher, A. (1964). Biogenic sedimentary structures. In: Approaches to paleoecology, Imbrie,]. and
N.Newell(ed0,pp·296-316.
Selli, R. (1973). An outline of the Italian Messinian. In: Messinian Events in the Mediterranean.
Geodyn. Sci. Rep., v. 7, pp. 150-172.
Simpson, S. (1957). On the trace-fossil Chondrites. Quarterly]. Geol. Soc. London, v. 112, n. 4, pp.
475-499.
Stanley, D. ]. (ed) (1972). The Mediterranean Sea: A natural sedimentation laboratory. Dowden,
Hutchinson and Ross, Inc., Stroudsburg, Penn., U.S.A.
Todd, R. and Low, D. (1966). Foraminifera from the Arctic Ocean off the Eastern Siberian coast.
U.S. GeoI. Survey, Prof. Paper 550-C, pp. 79-85.
Tolderlund, D. S. and Be, A. W. H. (1971). Seasonal distribution of planktonic foraminifera in the
Western North Atlantic. Micropal., v. 17, n. 3, pp. 297-329.
Uchio, T. (1960). Benthonic Foraminifera of the Antarctic Ocean. Seto Marine BioI. Lab., BioI. Results
of the Japanese Antarctic Res. Exp., Spec. Publ., v. 12.
Van Couvering, J. A., Berggren, W. A., Drake, R. E., Aguirre, E. and Curtis,]. H. (1976). The terminal
Miocene event. Mar. Micropal., v. 1, pp. 263-286.
Van Voorthuysen, ]. H. (1973). Foraminiferal ecology in the Ria de Arosa, Galicia, Spain. Zool.
Verh., v. 123.
Wall, D. (1962). Evidence from recent plankton regarding the biological affinities of Tasmanites
Newton 1875 and Leiosphaeridia Eisenack, 1958. Geol. Mag., v. 99, pp. 353-362.
Warme,]. E., Kennedy, W. J. and Schneidermann, N. (1973). Biogenic sedimentary structures (trace
fossils) in leg 15 cores. Init'l Rep. D.S.D.P., v. 15, pp. 813-831.

Wright, R. (1977). Neogene paleobathymetry of the Mediterranean based on benthonic Foraminifera
from D.S.D.P. leg 42 A. Init'l Rep. D.S.D.P., v. 42 (in press).
Zachariasse, W. J. (1975). Planktonic foraminiferal biostratigraphy of the Late Neogene of Crete
(Greece). Utrecht Micropal. Bull. II.
- Riedel, W. R., Sanfilippo, A., Schmidt, R. R., Brolsma, M. J., Schrader, H. J., Gersonde, R., Drooger,
M. M. and Broekman, J. A. (1978). Micropaleontological counting methods and techniquesan
exercise on an eight metres section of the Lower Pliocene of Capo Rossello, Sicily. Utrecht
Micropal. Bull. 17.

Fig. 1
Fig. 2
Figs.3a-b
Figs.4a-b
Figs. 5a-b
Figs.6a-b
Fig. 7
Fig. 8
Figs. 9a-b
Fig. 10
Fig. 11
Fig. 12
Fig. 13
Fig. 14
Fig. 15
Fig. 16
Fig. 17
Fig. 18
Fig. 19
Bigenerina nodosaria d'Orbigny, sample PP 33, X 100.
Eggerella bradyi (Cushman), sample PP 44, X 100.
Karreriella bradyi (Cushman), sample PP 33, X 100.
Vulvulina pennatula (Barsch), sample PP 18, X 70.
Bolivina alata (Seguenza), sample PP 48, X 65.
Bolivina antiqua d'Orbigny, sample PP 3, X 100.
Bulimina inflata Seguenza, sample PP 44, X 100.
Bolivina scalprata Schwager var. miocenica Macfadyen, sample CR 58, X 150.
Bolivina dilatata Reuss, sample CR 62, X 150.
Bulimina exilis Brady, sample PP 27, X 100.
Bulimina aculeata d'Orbigny, sample PP 48, X 100.
Bulimina costata d'Orbigny, sample PP 44, X 100.
Uvigerina peregrina Cushman, sample EM 43, X 100.
Uvigerina proboscidea Schwager, sample PP 44, X 65.
Uvigerina pygmea d'Orbigny, sample PP 44, X 65.
Hopkinsina bononiensis (Fornasini), sample PP 25, X 100.
Dentalinafiliformis (d'Orbigny), sample IT 1393, X 50.
Oolina hexagona (Williamson), sample CRP 12, X 150.
Nodosaria vertebralis (Barsch) var. albatrossi Cushman, sample CR 79, X 65.

Figs. 1a-b
Figs. 2a-b
Figs.3a-b
Figs.4a-c
Figs. 5a-b
Figs. 6a-c
Figs. 7a-b
Melonis barleeanus (Williamson), sample IT 1392, X 150.
Melonis soldanii (d'Orbigny), sample IT 1392, X 100.
Epistominella smithi (R. E. and K. C. Stewart), sample PP 25, X 150.
Epistominella exigua (Brady), sample EM 33, X 150.
Nuttallides rugosus (Phleger and Parker) var. convex us (Parker), sample IT 2056,
X 215.
Gyroidina orbicularis d'Orbigny, sample PP 44, X 70.
Gyroidina soldanii d'Orbigny, sample IT 1392, X 100; deformed specimen.
Figs.
8a-c
Gyroidina soldanii d'Orbigny, sample IT 1392, X 100.
Figs. 9a-c
Gyroidina umbonata (Silvestri), sample IT 1394, X 145.

Figs. la-b
Fig. 2
Figs.3a-b
Figs. 4a-c
Figs. 5a-b
Figs.6a-b
Figs. 7a-c
Figs. 8a-c
Figs. 9-10
Oridorsalis umbonatus (Reuss), sample IT 1393, X 100.
Oridorsalis stellatus (Silvestri), sample IT 1394, X 100.
Siphonina bradyana Cushman, sample pp 35, X 65.
Rosalinaglobularis d'Orbigny, sample IT 1390, X 150.
Globocassidulina subglobosa (Brady), sample IT 1394, X 150.
Ammonia beccarii (Linnaeus), sample CR 62, X 150.
Cibicides pseudoungerianus (Cushman), sample CR 62, X 150.
Hanzawaia boueana (d'Orbigny), sample EM 43, X 150.
Planulina ariminensis d'Orbigny, sample pp 44, X 65.

Figs. 1a-c
Figs. 2a-c
Figs. 3a-c
Figs.4a-b
Figs. 5a-c
Figs. 6a-c
Cibicides bradyi (Trauth), sample PP 1, X 100; Trubi-type specimen.
Cibicides bradyi (Trauth), sample PP 22, X 100; Narbone-type specimen.
Cibicides roberfsonianus (Brady), sample PP 22, X 65.
Cibicides italicus Di Napoli, sample PP 4, X 100.
Cibicides refulgens Montfort, sample CR 62, X 150.
Cibicides lobafulus (Walker and]acob), sample EM 43, X 150.

Pachysphaera. Small and large specimens. Large ones are always wrinkled, small ones
are mostly broken, sample CR 86, X 150 (figs. Ib and lc). Detail of fissure (fig. la,
X 1500) showing the delicate perforation of the wall.
Fig. 2
Figs. 3a-b
Fig. 4
Figs.5a-b
Bulimina elongata d'Orbigny, sample CRP 27, X 150.
Bolivina advena Cushman, sample CRP 37, X 300.
Oolina hexagona (Williamson), sample CRP 13, X 150.
Nuttallides rugosus (Phleger and Parker) var. convexus (Parker), sample CRP 21, X
380; fig. 5b (X 1100) shows some details of the aperture extending parallel to the
periphery.

Fig. 1
Fig. 2
Figs.3a-b
Fig. 4
Fig. 5
Fig. 6
Fig. 7
Fig. 8
Fig. 9
Globigerina bulloides d'Orbigny, sample PP 40, X 75.
Globigerina apertura Cushman, sample PP 32, X 75.
Globigerinafalconensis Blow, sample CRP 18, X 75.
Globigerinoides obliquus Bolli, sample PP 40, X 75.
Globigerina quinqueloba Natland, sample PP 40, X 150.
Globigerinitaglutinata (Egger), sample PP 40, X 150.
Globigerinoides extremus Bolli and Bermudez, sample PP 40, X 75.
Globigerinoides trilobus (Reuss), sample PP 40, X 75.
Globorotalia margaritae Bolli and Bermudez, sample CRP 32, X 75; thick-shelled
specimen from non-laminated Trubi interval.
Globorotalia margaritae Bolli and Bermudez, sample CRP 29 A, X 75; thin-shelled
specimen from the fourth laminated Trubi interval.
Fig. 11
Fig. 12
Fig. 13
Fig. 14
Fig. 15
Fig. 16
Fig. 17
Fig. 18
Fig. 19
Globigerinoides sacculiferus (Brady), sample PP 40, X 75.
Globigerinoides ruber (d'Orbigny), sample PP 40, X 75.
Globigerinoides elongatus (d'Orbigny), sample PP 40, X 75.
Globorotalia subscitula Conato, sample PP 40, X 150.
Neogloboquadrina acostaensis (Blow), sample PP 40, X 150.
Globigerina pseudobesa (Salvatarini), sample PP 40, X 75.
Globorotalia crassaformis Gallaway and Wissler, sample CR 154, X 75.
Globorotalia crassacrotonensis Canata and Folladar, sample PP 18, X 75.
Globigerina pachyderma (Ehrenberg), sample PP 44, X 150.

Variation of Globorotalia puncticulata (Deshayes) in the assemblage from sample
CR 43, X 75.
Intergradation of Globorotalia puncticulata (Deshayes) into Globorotalia bononiensis
Dondi, in successive assemblages from the Punta Piccola section, samples PP 4, 6, I1
and 20 corresponding to figs. 2,3,4 and 5, respectively; X 75.
Variation of Globorotalia bononiensis Dondi in the assemblage from sample PP 36,
X 75.

Morphological gradation from Globorotalia bononiensis Dondi to Globorotalia inflata
(d'Orbigny) in successive assemblages from the Punta Piccola section, samples PP 40,
45 and 47 corresponding to figs. la-2f, 3a-4f and 5a-6f, respectively; X 75.

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