professor liviu ionesi`s contributions to the paleogeographical

ACTA PALAEONTOLOGICA ROMANIAE V. 6 (2008), P 97-103.
PROFESSOR LIVIU IONESI’S CONTRIBUTIONS TO THE PALEOGEOGRAPHICAL
EVOLUTION OF THE EASTERN CARPATIANS FORELAND KNOWLEDGE
Petru ENCIU1 & Cristina DUMITRICĂ1
Abstract
Academician Liviu Ionesi has published between 1964-1972 and 1991-1996 many papers regarding the
paleogeographical evolution of the Eastern Carpathians foreland, as result of the cooperation with doctor in
geography and university professor Nicolae Barbu and with doctor emeritus professor Bica Ionesi, specialist
in paleontology. The contribution of the first stage was based on the lithological, internal mechanical
structures and fossil fauna content (age and facieses markers) studies. The existence of some sedimentary
gaps for Upper Kossovian – Early Buglovian, Early Basarabian and part of Hersonian intervals, sustained by
the authors, are based on fauna analysis of Badenian – Maeotian deposits.
Then, between 1996-2005, continuing the second stage of researches in this field, academician Liviu Ionesi
together with a group of four authors has synthesized a good part of the paleogeographic elements in a
paper dedicated to the Middle and Upper Sarmatian of Moldavian Platform.
In this second stage, the researches were diversified and the results were obtained mainly from the modern
interpretation of the biofacies significance, constructed by foraminifers, bivalve mollusks, gastropods,
marine vertebrates or terrestrial vertebrates. For the western strip of the Moldavian Platform, new
arguments were presented regarding the existence, even in Volhynian, of a mature courses network
originated in the emerse terrains of the Eastern Carpathians with the solid burden deposited as deltas and
littoral deposits in the coupling zone with the Moldo-Galitian Gulf.
In the monographic paper dedicated to Medium and Upper Sarmatian period, published in 2005, for each of
the 12 component formations, sedimentological and paleontological considerations were presented and 5
significant paleogeographical stages were separated for the whole Badenian- Romanian sedimentary cycle.
Keywords: Carpathians, Moldavian Platform, Miocene, Pliocene, paleogeography.
INTRODUCTION
The paper was presented on September
2007 at the scientific workshop of the
Romanian Paleontological Society as homage
to academician Liviu Ionesi who passed away
almost a year ago.
The geological community is well aware of
Liviu Ionesi contributions regarding the
northern part of the Eastern Carpathians flysch
formations stratigraphy and tectonics, an
activity developed on a large period (1950 –
1968). But even in the years of intense efforts
for Eastern Carpathians geology knowledge,
together
with
other
geological
and
geographical researchers, Liviu Ionesi had a
constant interest in paleogeographical field,
rewarded with important results.
SHORT HISTORY OF RESEARCHES
In case of structural units situated in front
of the Eastern Carpathians, the first reference
regarding the paleo-geographical conditions
during Miocene – Present time dated in the
second decade of the XX-th century (David M.,
1916).
A brief analyze of the papers elaborated
after, for about nine decades, indicate the
existence of four stages. In each stage the
paleogeographical approaches were based on
information from related fields and the results
were dependent on the general evolution in
bio- and geo- sciences.
Here is a condensed characterization of
each stage:
1. The first stage is one of punctual
remarks, especially about the paleo-climate
1 Institute of Geography, Romanian Academy, Bucharest
and was based on the studies of leafs prints
founded in rocks of different ages; David M.,
1916; Simionescu I. 1927; Barbu I. Z., 1934,
etc.
2. Using combined morphogenetic and
stratigraphic arguments, the second is the
stage of age estimation for the Eastern
Carpathians hydrographic network and for the
associated accumulative relief built at the
transition zone to the foreland. Here we have
the papers signed by Martiniuc C. (1948);
Tufescu V. (1957); Barbu N., Ionesi L., Ionesi
Bica (1966), Donisă I., Barbu N., Ionesi L.
(1973), etc.
3. The third is dedicated to the relief
evolution of the structural units situated in front
of the Eastern Carpathians. Main contributions
are considered the paper of Sficlea V. (1980)
for Covurlui Platform, others, signed by Ionesi
L., Barbu N. and Ionesi Bica (1991, 1993),
regarding the weathering model upon the
Carpathians foreland in Badenian and
Sarmatian time, or about the Moldavian Plain
Genesis (Ionesi L., Barbu N. 1996), etc.
4. The stage regarding the sedimentation
conditions and the depositional ambiances
obtained by detailed analysis of the internal
structures and the sedimentary rocks
petrography (Miclăuş Crina, 2001; Grasu C.,
Miclăuş C., Brânzilă M. & Boboş I., 2002). In
the same stage, paleoclima studies diversify
using spore – pollen analysis on large sets of
clays samples deposited in Basarabian time:
Ţabără D. and Olaru L., 2004; Brânzilă M. and
Ţabără D., 2005, etc.
97
P. ENCIU & C. DUMITRICĂ
MAIN PALEOGEOGRAPHIC STAGES
In
the
paleogeographical
evolution
knowledge field of the Moldavian, Barlad and
Covurlui Platforms that evolved as a single
block
between
Middle
Miocene
and
Quaternary, Liviu Ionesi’s contributions are the
result of a complex team work.
In the first interval the work was done
together with Nicolae Barbu and Bica Ionesi
(1964, 1966, 1972, etc.). After 1989 in this
team were included researchers as Vladimir
Roşca and Alexandru Lungu from the Republic
of Moldavia. The results of this long
collaboration were fructified in 2005. In the final
part of the most valuable geological study
dedicated to the Middle and Upper Sarmatian
of the Moldavian Platform, the main positive
oscillations of the basement (generating land),
and implicitly, the main morphogenesis stages
were presented (Liviu Ionesi and contributors,
2005).
These will be presented in the following
paragraphs.
1. Weathering Model – Dorohoi Surface
After Cretaceous (in the eastern part) and
after Middle or Upper Eocene (in the western
part), most of the foreland units become land
for about 40 Ma (Ionesi, 1984), been a
sediments
source
for
the
carpathic
geosynclinal (on the west). In this considerably
long time range, a weathering modeling of the
cretaceous, eocene and paleozoic deposits
took place. Now it was mould the Dorohoi
peneplene surface. It has a plain character
and it was crossed by a network of valleys with
NE – SW orientation in the northern part of the
platform, and E – W in the southern part;
valleys marking the ditch of the Carpathian
geosynclinal (Paraschiv, 1987).
2. The New Stiric orogenetic phase from
Upper Badenian
Now, the Dorohoi Surface was buried and
deformed gradually by the western plunging; a
process more obvious to the west of the Siret
valley. Do to the eastern thrusting of the
carpathian units, the western margin of the
Dorohoi Surface was masked by tectonic
covering, presently been situated at about 50
km west of the pericarpathic line.
That means a 50 km shortening of the
alpine formations stack in Carpathians, their
thrusting over the Moldavian Platform and the
differentiated subsidence of the latest with
accumulation of three Badenian formations:
detritic, anhydrite and marl-argillaceous (see
Figure 1). Analyzing the basement position,
Ionesi et al., 2005, sustained that the bending
98
of the platform to south and west is tectonic,
possibly along some fractures. Isobaths to the
base of Badenian are 0 – 100 m to NE and at 1500 m in front of the orogene (Ionesi, 1994).
Under the orogene, the depth of the above
mentioned limit grows abruptly to 2000 and
5000 m.
3. Formation of the Moldo-Valachian
Land between Kossovian and Early
Buglovian
Between Kossovian and Early Buglovian,
~14 – 13.8 Ma BP, the Subcarpathian Nappe
was put in place. The uplift can be linked with
the Moldavian (Attic) Phase of the Carpathian
alpine cycle. This process affected the whole
foreland of the Eastern and Southern
Carpathians, inclusively the South Dobrogea
and the centre of the Valachian Platform, and
has generated among others the Moldo-Valach
land (Ionesi L., Barbu N. & Ionesi Bica, 1991).
The Moldavian Orogenetic Phase has
stimulated the generation of a hydrographic
network and landforms into Carpathians. The
maximum erosion value, ~ 0.5 mm/year, took
place at about 13±0.2 Ma. At the river courses
outlet, piedmont cones on the land (Clit, Ciungi
a.o.) and deltas at the entrance of the MoldoGalitian Gulf, were formed.
4. A marine transgression in Upper
Buglovian
The moldo – valachian land was buried
after the sedimentation was restored in Upper
Buglovian time, when a new marine
transgression has covered Moldavian and
Barlad platforms, part of the Covurului
Platform, north and west of the Moesian
Platform, as well as South Dobrogea. As a
consequence of the piroclastic emissions of
the Carpathian Volcanic Chain, Hudesti dacitic
tuff was deposited (see Figure 1).
5. Intra – Volhynian orogenetic phase.
Now is the time of the final put in place of the
Subcarpathian Nappe. The thrusting process
of the foreland (Maţenco et al. 2003) was
blocked first north of the Bistrita fault and then
between Bistrita and Trotus faults. South of
Trotus,
Subcarpathian
Nappe
plunges
progressively,
generating
the
Odobesti
depositional area; a high subsiding basin
during Upper Sarmatian – Middle Romanian
time.
The Moldavian Orogenetic Phase (12.5 Ma)
has generated trusting and shortening of the
Carpathians Units, with a litostatic overburden
and a subsidence on the western edge of the
PROFESSOR LIVIU IONESI’S CONTRIBUTIONS TO THE PALEOGEOGRAPHICAL EVOLUTION
OF THE EASTERN CARPATIANS FORELAND KNOWLEDGE
Figure 1 – Foreland’s stratigraphic synthesis during Middle Miocene – Holocene time
(ro3 – Upper Romanian; ro2 – Middle Romanian; ro1 – Lower Romanian; P1-2 - Pontian; m Maeotian;hs - Hersonian; bs - Basarabian; vl - Volinian; b - Buglovian; bn – Badenian; 15.0…1.8
million years BP)
99
P. ENCIU & C. DUMITRICĂ
platform units, configuring the Carpathian
Fore-deep.
On the north – western edge in Upper
Volhynian time dryness has appeared and
prolonging them, low plains with marshes (now,
three coal layers). The vegetation (grass and
broadleaves woods mixed with mediterranean
species) denotes a humid temperate climate (in
transition to sub-tropical). Generally, Volhynian
age has 150 m thickness east of Siret valley,
500 m between Siret and Moldova rivers and
800 m in front of the Carpathians Chain,
indicating a differentiated plunge.
6. Volhynian – Lower Basarabian
Between Volhynian and Lower Basarabian
time at the contact zone of the Carpathian land
and the Sarmatian Sea, hydrographic courses
existed: paleo-Suceava, paleo-Suceviţa, paleoMoldova, paleo-Ozana, paleo-Cracău, paleoBistriţa, etc. The Upper Buglovian – first part of
Basarabian paleogeographic evolutionary time
was called Bahlui. This range is characterized
by two reefs barriers in the eastern part. The
first Buglovian barrier has extended from south
of Iasi till Podolia and the Late Volhynian –
Early Basarabian barrier was installed east of
the first one. The two barriers and the sandy –
limestone layers reveal the oscillating levels of
Moldavian Platform (n.n. – induced by Planetary
Ocean’s oscillations).
7. The general uplift of the Moldavian
Platform from Upper Basarabian
The
sedimentation
was
maintained
constantly until the first part of the Upper
Basarabian when a tectonic uplift process
(without any folding effects) and land
generation took place. The limit between the
land, build in the northern part, and the aquatic
basin, from south, was the trace of the N
Roman – Oţeleni – Iaşi – Făleşti fracture,
named Bahlui fault (David, 1922), with a
prolongation east of Prut valley.
With this differentiated uplift, more important
in the north, important changes are made.
Water’s freshening was the first important
consequence. Information are supplied by the
Upper Basarabian deposits, with Mactra
macarovicii, congerias and layers with freshwaters fauna between Clays with Criptomactra
pesanserii and the Repedea Limestone (Ionesi,
1993). In the same period Crimeea – North
Dobrogea barrier was uplifted, isolating the
Moldo – Galitian Gulf from the Euxinic Basin.
The marine – brackish waters retreated in
the north as a consequence of the uplift, leave
a plain land on which the hydrographic network
was developed. Over the Criptomactra
Formation and Darabani – Mitoc clayey Beds
will flow the Upper Basarabian paleo – Bahlui,
100
paleo – Jijia and is installed the Prut valley
(Ionesi et al., 2005).
It cannot be excluded that Jijia, Bahlui and
Prut (north of Bahlui fault), Rautz, Cubolta and
Cainar valleys to be the heirs of this network.
The land remains the same till now. On the
land vegetation developed and a community
of herbivores and carnivores, known as
Hipparion moldavicum fauna, lived.
On foreland’s western edge, the paleo –
hydrographic networks of the actual Siret,
Suceava Sucevita, Solonet, Moldova, Suha,
Ozana and Cracau courses drains the
Carpathian land. Ionesi and Barbu (1996)
consider that by the union of this courses the
medium course of Siret was build. On its right
side, between Toplita and Bistrita valleys, an
Upper Basarabian land (without the
accumulation of
Barnova – Muntele
Formation) existed. The structural researchers
say that in the Upper Basarabian the
subsidence was blocked/stopped in a strip
north of Trotus, and sedimentation process on
the frontal platforms of Eastern Carpathians
was mainly under a N – S control (Maţenco &
Bertotii, 2000).
8. Reneweing the link with the
Sarmatian Sea
In the south – central part of Moldavian
Platform, after the accumulation of small
mactras and congerias deposits, the link with
the Sarmatian Sea was restored. In the
aquatic area, named by the authors the Moldo
– Galitian Gulf, marine – brackish waters
enter (with Mactra fabreana, M. vitaliana, M.
podolica) and a severe reduction of the
terigene material input took place. This stage,
named Repedea, ended in Late Basarabian.
As a consequence, Repedea, Şişcani, Şcheia,
Bălăneşti, Măgura, Bujor, Lăpuşna and
Bohotin formations resulted (see Figure 1). By
the lithology (oosparite, biosparite, sands), by
the structure (wave ripples, rib and furrow,
oblique – crossing bedding) and by faunal
composition, there are littoral formations. An
additional argument is the presence of the
terrestrial (Helix) and fresh-waters (Anodonta,
Unio, etc.) mollusks transported from the
nearby land.
9. Reduction of sedimentation area
Due to the Carpathians geodynamic
processes, at the Basarabian - Hersonian
boundary, approximately between 11.0 – 10.8
Ma BP, the whole foreland, inclusively the
strip of the Black Sea shelf, was emerged.
Then, in Hersonian time, the south central part, approximately between the Paun
and Barlad localities meridians, was
dominated by a delta environment (Valeni
sands).
PROFESSOR LIVIU IONESI’S CONTRIBUTIONS TO THE PALEOGEOGRAPHICAL EVOLUTION
OF THE EASTERN CARPATIANS FORELAND KNOWLEDGE
The salinity diminishes, generating the
extinction of Mactra fabreana fauna and the
installation of small mactras fauna. Beside the
small mactras fauna, deposits with fluviallacustrine and terrestrial fauna (Balta – Paun
Formation) are preserved. Because of the
intense volcanic activity from the Calimani
Mountains, are accumulated also Nutasca –
Ruseni cinerites (an important stratigraphic
marker).
Sedimentation continues between Maeotian
– Middle Pontian time, been preponderantly
epiclastic (sands, sandstones, silts and,
subordinated, clays). The weakly brackish
waters regime permits development of some
species as Congeria panticapaea, Dosinia
meotica,
Syndesmia
tellinoides,
Unio
moldavicus, etc., and on land mammals of
warm climate that lived in luxurious vegetation
conditions (Ionesi, 1994).
From the rocks deposited in Maeotian are
known three outcrops with flora (Păun-Iaşi,
Hârşova-Vaslui and, possibly, Nisporeni) from
which were identified taxons of warm and
humid, almost subtropical climate (Laurus,
Cinnamophyllum, etc.); character proved also
by the vertebrate remains.
The fauna deposit of Cimislia contains
proboscideans (Zygolophodon, Tetralophodon,
Deinotherium giganthissimus Ştefănescu, D.
longirostris), birds (Struthio), carnivores and
many herbivores.
Regarding the Pontian time, Ştefârţă Ana
(in: Ionesi et al., 2005) presents some data of
paleo-flora from the outcrops Moscova and
Taraclia. The presence there of some species
of Parrotia, Betula, Salix, Acer, Typha, etc.,
denote a warm towards subtropical climate.
10. Development of the emerged territory
After
Middle
Pontian,
important
paleogeographic changes took place, as in
case of land development. Authors sustain that
the enlargement of land happened as a
consequence of the general uplift process. Is
not impossible that the waters retreat to be a
result of the general climatic depreciation and
descend of the Dacic Basin’s water level, too
(Clauson et al., 2005).
As the authors, Ionesi et al., 2005, sustain
the new land has higher levels than the existent
one north of Bahlui fault. Consequently, Bahlui,
Jijia and Rautz valleys arcuates toward Prut
River. From the whole generation of valleys
installed on the southern bench of the
Moldavian Central Plateau, only Rautz has
penetrated.
As concerns the Pontian deposits, they are
missing from the Moldavian Platform, been
present south, on the Scythian (Barlad)
Platform. There, Lower and Middle Pontian
are represented by continental deposits
(latheritic clays and red siltstones like residual
products in the continental temperate, more
humid climatic conditions).
11. The Malusteni stage was developed
in Dacian – Middle Romanian time. Now,
south of the Crăieşti – Fălciu – N Comrat –
Căuşeni line it was a lake. In this lake were
accumulated Malusteni – Beresti Formation,
followed by Balabanesti Formation.
The first formation has alluvial sands with
many mammals (Terzea, 1981). Based on the
mammals association, the Beresti fauna is
attributed to Upper Dacian, and the Malusteni
one with rodents, lagomorpha, medium and
big herbivores, associated with carnivores
and monkeys, is attributed to Lower
Romanian. Judging after the thanatocenozes
composition, the climate was warm and humid
(almost subtropical), with herbal abundant
vegetation, but also with forests.
The next formation, Balabanesti, starts
with gavels (5 – 10 m thickness) with
lithoclasts of Carpathian’s origin in base,
followed by sands (30 – 50 m). Here the
contribution of Siret, Bistrita and Trotus rivers
was highly.
12. The Valachian Orogenic Phase that
followed during the Upper Romanian-Lower
Pleistocene, generates an uplift of the
Moldavian, Barlad and Covurlui Platforms,
more important to NW, and reduced to SE.
That explains the actual arrangements of all
formations
inclusively
the
Balabanesti
Formation (oriented WSW – ENE and having
SE bending of 6 – 8 m/km).
The area of the existed Malusteni Lake
becomes land. The upper course of Barlad
River outlet into Prut and the lower course
was deviated toward Siret due to the Focsani
high subsiding area.
13. Thanks to an ingression of the Black
Sea into the actual territory of Romanian Plain
in Middle Pleistocene time, Babele – Barbosi
Formation was accumulated, with fluvio –
lacustrine (Corbicula, Pisidium, etc.) and
brackish marine mollusks (Didacna, Adacna,
etc.).
14. Over the all presented base
formations, one mainly aeolian Loess
Formation was accumulated (with loess,
loess-like, fossil soils, etc.). This formation is
variable in thickness from some meters in the
north (the Moldavian Plain) till fifty-sixty
meters in the south (Galati or Covurlui Plain).
101
P. ENCIU & C. DUMITRICĂ
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