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ed. These fossils are more abundant in the upper part of the A member, which illustrates the abundance and diversity in C1 and C3 sub-members belonging to the C member. To classify these samples, classical and up-to-date methods were used. However, the systematic schemes were used more frequently (Moore, 1966
cadas por medio de los métodos recientes y clásicos. Sin embargo, los esquemas sistemáticos fueron usados con más frecuencia (Moore, 1966
co y el mar Mediterráneo.
Voir plus Voir moins

Earth Sci. Res. J. Vol. 11, No. 1 (June 2007): 57-79
Keyvan Khaksar
Islamic Azad University, Qom, Iran. k1khaksar@yahoo.com
Iraj Maghfouri Moghadam
Lorestan University, khorram- Abad, Iran. Irajmmms@yahoo.co.uk
The Qom formation was formed in the Oligo-Miocene during the final sea transgression in Central
Iran (Figure 1). The best outcrop is located in the vicinities of the Qom City, approximately 130
km at the south of Tehran. In general, the great heights of the zone are the result of intense tectonic
activities. These heights have a number of faults and folds. Echinoderms are one of the most
important and numerous fossil groups present in the Qom Formation and confirm the relationship of
this environment with free waters. In the investigation more than 100 prepared samples were
studied and 17 species were identified, scanned and classified. These fossils are more abundant in the
upper part of the A member, which illustrates the abundance and diversity in C1 and C3 sub-members
belonging to the C . To classify these samples, classical and up-to-date methods were used.
However, the systematic schemes were used more frequently (Moore, 1966; 1969-1971).
Besides these studies, the other concomitant microfossils in the formation were investigated
simultaneously to estimate the accurate age of them. It is concluded that the study of Oligo-Miocene
Echinoderms present in the Qom formation is essential and important because, at the same time, the
Central Iran Sea had a communicative role between the Indo-Pacific Ocean and the Mediterranean
Key words: Central Iran, Oligo-Miocene, Limestones, Echinoderms.
La Formación Qom se formó durante el Oligoceno-Mioceno durante la transgresión final del Mar
en Irán Central (Figura 1). El mejor afloramiento se encuentra localizado en los alrededores de la
ciudad de Qom, aproximadamente a 130 km al sur de Teherán. En general, los altos pronunciados de
la zona son el resultado de la intensa actividad tectónica. Estos altos poseen un gran número de fallas
y pliegues. Los Equinodermos son los fósiles más importantes y numerosos que se encuentran en la
Formación Qom y confirman la relación de este ambiente con el agua. En la presente investigación
más de 100 muestras fueron preparadas y estudiadas, y de las mismas se identificaron y clasificaron
Manuscript received December 15 2006.
Accepted for publication June 10 2007.

57Paleontological study of the Echinoderms in the Qom Formation
(Central Iran)
17 especies. Esto fósiles son más abundantes en la parte superior del miembro A, el cual ilustra la
abundancia y diversidad en los sub-miembros C1 y C3 pertenecientes al C. Estas muestras
fueron clasificadas por medio de los métodos recientes y clásicos. Sin embargo, los esquemas
sistemáticos fueron usados con más frecuencia (Moore, 1966; 1969-1971).
Aparte de estos estudios, los otros microfósiles concomitantes en la formación fueron investigados
simultáneamente para estimar su edad exacta. Se concluyo que el estudio de los Equinodermos del
Oligoceno-Mioceno presentes en la Formación Qom es esencial e importante porque, al mismo
tiempo, el mar de Irán Central permitía la comunicaión entre el océano Indo-Pacífico y el mar
Palabras Clave: Irán Central, Oligo-Mioceno, Calizas, Equinodermos.
INTRODUCTION in this part are benthonic and planktonic
The Marine Qom Formation was deposited in
the Oligo-Miocene and is the result of the last C Member
transgression of the sea in Central Iran. The The C Member has an average thickness of 370
formation contains five members containing meters and has the following sub-members:
limestone interstratified with marlstone and
deposited during three sedimentary cycles. The C1: Composed by marlstones interstratified
mean thickness of this formation is approximately with limestones. The thickness of the bed is
900 meters in the vicinities of the Qom City. This between 10 and 200 cm. The limestones have the
formation consists of the following five members following texture starting from the base:
(Figure 2): • Packstone with abundant fossil assemblages
of echinoderms, bivalves, bryozoans, red
A Member algae, gastropods, and corals.
The A Member has an average thickness of • Boundstone containing bryozoans, corals,
55 meters and the thickness of its beds varies and red algae.
between 2 and 200 cm. This member contains
several parts starting from the base: C2: C2 illustrates the termination of the primary
sedimentary cycle. It contains the following
• Limestones with muddy texture without textures:
fossils. • Mudstones with plenty of organic materials.
•(packstone) containing benthonic • Layers of gypsum.
• Limestones (grainstone) containing oolits C3: This sub-member is composed by limestones.
and bioclasts. The thickness of the bed is between 5 and 300 cm
•(packstone) with foraminifers, and composed by the following textures starting
bryozoans, red algae, gastropods, bivalves, from the base:
and echinoderms. • Grainstone containing oolits, bioclasts,
• Sandstones with glauconite containing and sedimentary structures such as
crossremnants of complete echinoderms, bedding.
bryozoans, and sedimentary structures such • Packstone and boundstone with echinoderms,
as cross-bedding. corals, bryozoans, and red algae.
• Packstone with shell fragments of bivalves
B Member and foraminifers.
It is composed by 225 meters of thick layers of
sandy marlstones and sandstones intercalations C4: Composed by marlstones containing
(with cross-bedding) and containing glauconite, foraminifers, corals, and internal moulds of
which is the cause of the green colour of gastropods. Catapsydrax stainforthi BOLLI,
marlstones. The fossils commonly observed LOEBLICH, and TAPPAN are also found in this

58Khaksar and Maghfouri, ESRJ Vol. 11, No. 1. June 2007
Figure 1. Distribution of Oligo - Miocene marine sediments in Central Iran..
sub-member belonging to Burdigalian.
D Member
This member illustrates the Qom Formation’s Because of macro and microfossils of the Qom
second termination cycle and consists of 22 Formation such as Globorotalia (Turborotalia)
meters thick layers of gypsum. opima opima BOLLI present in the member
B and Catapsydrax stainforthi present in the
E Member C member. This formation has been known
It is composed by 230 meters of thick layers chronologically.
of marlstone intercalated with limestone. The
fossils commonly observed are: foraminifers, red Figure 3 shows the vertical distribution of
algae, gastropods, bivalves, and bryozoans, with echinoderms. The existence of some Echinoderms,
following textures (limestone) from the base: Echinodiscus balestrai and Clipeaster folium
• Packstone with bryozoans, red algae, MICHELIN, in the lower part of the formation
gastropods, and corals gives it an age of Medium-Superior Oligocene.
• Boundstone containing stromatolites, corals,
and bivalves The decrease in the number of Echinoderms
• Grainstone containing bivalves, red algae, towards the upper part of the formation is due
and benthonic foraminifers. to the great migration of these species towards

59Paleontological study of the Echinoderms in the Qom Formation
(Central Iran)
Figure 2. Stratigrafic section of the Qom Formation.

60Khaksar and Maghfouri, ESRJ Vol. 11, No. 1. June 2007
Figure 3. Vertical distribution of Echinoderms in the sediments of the Qom Formation.
the North in Burdigalian sup. because Earth’s already erosive. This can be seen in sandstones of
temperature was generally high in Burdidaliense the upper member A and sub-member C1. These
(Demarcq, 1984). However, the temperature in layers demonstrate turbulent movements at the
Burdigalian sup. rose even further (Flower and bottom of the sea. This secondary echinoderm
Kennet, 1994). accumulation illustrates the periodic sea storm,
which causes erosion of fine sediments and
TAPHONOMY echinoderm fragment accumulation (Figure 4).
In several places of Central Iran, the layers are Due to the irregular base of the layers, each bed
steeps because of folding and tectonic activities, could be originated from remaining sediments
and it takes a long time to identify top and (lag) of turbulent sea beds, demonstrating a
bottom sedimentation layers. In these cases, transgressive phenomenon in the sedimentary
the presence of echinoderms is one of the best basin.
criteria to recognize the polarity and also reflects
a calm sedimentary environment. GEOLOGICAL SETTING
Sometimes, it could be observed that the The Qom province is part of the Central Iran
layers, exclusively composed by this genus zone, in which sub-parallel mountain ranges and
of echinoderms (Scutella and Clypeaster), are plains have general northwest-southeast trend.

61Paleontological study of the Echinoderms in the Qom Formation
(Central Iran)
Figure 4. Formation of beds made of Scutella fossils.
The North-western plain is the terminal part of this period volcanic activities continued locally,
the Qom-Ardekan depression, divided into two represented by analcite bearing basanite and
parts by the small hills of the Koshk-e-Nosrat andesites. In the Late Miocene, thick
lagoonalheights located to the north of the Howz-e- continental deposits of Upper Red formation
Soltan Lake. The Central parts of the province were replaced by the marine Qom
have hillocky topography, while the western with two distinct Neogene volcanic activities
and southwestern parts are mountain regions (Bozorgnia, 1965).
belonging to the Urumiyeh-Bazman volcanic
belt, with some summits up to 3000 meters. Pliocene sequences of Qom formation have
various facies. They are comprised by three
The oldest known rocks of this province are of volcanic-subvolcanic, volcanic-sedimentary and
Eocene age, which are younger volcanic rocks detritical units. Plutonic igneous bodies, which
exposed in western parts of this province and intrude into the Urumiyeh-Bazman volcanic
belong to the Urumiyeh-Bazman volcanic belt. rock, are other characteristical feature of the
These magmatic rocks can be divided into three Qom province. These intrusive bodies have
zones: Ashtian-Naragh, Tafresh and Saveh. The definitively a conspicuous relation with fracture
Tafresh member has a central position with zones. The intrusive bodies are either extensive
respect to Ashtian-Naragh (south) and Saveh or small.
(north) members. This part is characterized by
an important sedimentation and subsidence The Qom province is still an active tectonic
while the Saveh member is by environment materialized by active seismicity.
important Upper Eocene magmatic activity, and The late movements, with general direction
the Ashtian-Naragh member is featured by its of north-northeast compression, configure the
high volcanic activities of the Neogene. actual structural feature of this province.
Orogenic movements in the Late Eocene-Early PALEOGEOGRAPHY
Oligocene resulted in the creation of lagoonal to
continental sedimentary regime characterized by Considering the results of the present study
detritic-evaporitic sediments of the Lower Red and those of the previous works in the
Oligoformation. Local and lateral facies changes are all Miocene outcrops in different regions of Iran
related to inherited local changes of topography. and their environments, it is attempted here to
Lagoonal evaporites of rather considerable reconstruct the paleogeography of this region.
thickness represent high rate of subsidence in As a result of the tectonic movements of the
this continental environment (Tehrani, 1989). upper Cretaceous and the rise of Northern region
of the Alborz (Tehrani, 1989), two different
Oligo-Miocene carbonates of the Qom formation sedimentary basins have been formed: one in the
represent marine transgressions in this province North of the Alborz (Pentocaspiana basin) that is
with marly-calcareous sedimentation. During situated in the present zone of the Caspian Sea,

62Khaksar and Maghfouri, ESRJ Vol. 11, No. 1. June 2007
and the other is located in the Southern part of PALEOCLIMATOLOGY
the same mountain range (in Central Iran). In
central Iran, the Eocene and Lower Oligocene Skeletal and non skeletal sediment particles were
are characterized by continental sediments studied and could be summarized as follows:
(Lower Red Formation). The basal contact of
the transgressive deposits of Oligo-Miocene age SKELETAL PARTICLES
with the L.R.F. is marked in many zones by an
angular discordance that indicates the influence The large number of fauna such as corals and
of the tectonics movements before the marine macroforaminifers in upper parts of the C
transgression (Bozorgnia, 1965). and E Members indicate high temperatures.
Macroforaminifers in the Qom Formation such
During the Oligocene (Chattian) a great channel as Operculina, Miogypsina, Miogypsinoidi,
connecting the Mediterranean and the dominion Lepidocyclina, Heterostegina, Amphistegina,
Indian-Pacific through the South of Iran was and Spiroclypeus are representative of warm sea
formed, separating Africa and Euro-Asia. In the environments (Boltovskoy and Wright, 1976;
Miocene (Burdigalian), rotations and vertical Allasinaz, 1983; Demarcq, 1984; Lauriat et al.,
and horizontal movements of the Lut block 1993).
and Arabian plate, and the impact between
the latter with Turkey, caused the interruption The presence of Rotalia viennoti and Borelis in
of connection between the Mediterranean limestones illustrates tropical climates (Delanoe
and the Indian Ocean during the Burdigalian et al., 1976; Lauriat et al., 1993). The Presence
(Steininger and Rogl, 1984). The sea invaded of Red Algae (Lithophylum, Mesophyllum,
a part of Turkey (Adana and Karaman), where Sporolithonn, and Lithothamnium) also
the outcrops are formed generally by limestones represents tropical climate (Bosence, 1983).
with Lithothamnium. In Syria, the deposits of
the Burdigalian have high contents in Pecten, Macrofossils such as Scutella, Clypeaster,
Clypeaster, and macroforaminifers. The extension Echinolampas, Amphiope, and Maretia represent
of these deposits covers a large area of Syria and warm waters. Maretia is an indicator of tropical
from Mesopotamia to Iraq, and from there to the climates, as observed in the Indian and Pacific
Persian Gulf. These indicate that a sea passage domains (Llompart, 1983; Lauriat et al., 1993).
existed between the Mediterranean and the Indian The presence of bio-constructions and hermatipic
Ocean. This channel was interrupted in the upper corals in several layers (e.g., upper layers of the
Burdigalian because of the orogenic movements C1 submember) confirms that the temperature
o othat affected the Mediterranean coasts and Iraq. ranged from 18 to 30 C (Minnery et al., 1985).
In the northern zone of the Mediterranean, the The presence of bivalves such as Amusium
Rzehakia (Oncophora, Bivalvia) marine series, and Spondylus is representative of warm sea
containing molluscs of the Burdigalian, are environments (Demarcq, 1979; Turek et al.,
extended from Switzerland to the Aral Sea. They 1988).
are attributed to shallow basins, which are isolated
and interconnected by a partial connection with NON-SKELETAL PARTICLES
the open sea and influenced by continental
environments. The Langhian is characterized by These particles such as oolits indicate warm
great geodynamical instability and a sediment and dry climates belonging to sea environments
substitution of the shallow marine condition where evaporation exceeds rainfall (Reijers et
by continental sediments in the Arabian plate al., 1983; Zeng et al., 1983).
oand Mesopotamia (Buchbinder and Gvirtzman, Oolits are formed at temperatures above 15 C and
1976). The last marine regression took place minimum salt content of 36 percent (Lees, 1975).
during the Langhian in central Iran. It seems that after the cold Lower-Oligocene,
the temperature in the Superior-Oligocene
increased, reaching its optimal temperature in
the Burdigalian. Then, the suffers

63Paleontological study of the Echinoderms in the Qom Formation
(Central Iran)
a sudden decrease in the Middle Miocene • The presence of corals and foraminifer
(Demarcq and Pouyet, 1990). fossils represents warm climates.
In conclusion, it could be understood that the
sediments of the Qom Formation were formed in SYSTEMATIC
tropical and subtropical environments.
CONCLUSIONS Subclass Euechinoidea
Superorder Gnathostomata
• Firstly, the presence of Echinoderms in the Order Clypeasteroida
Qom Formation reveals a passage to the Suborder Clypeasterina
sea. Family Clypeasteridae
• The presence of Echinoderms in the Qom Genus Clypeaster LAMARCK, 1801
Formation is one of the best criteria to Clypeaster aff. scillae DESMOULINS
recognize polarity and also reflects a calm Pl.1, fig.1
sedimentary environment.
• The presence of the Echinodiscus balestrai 1837 Clypeaster scillae DESMOULINS, p.64.
OPPEN and Clipeaster folium MICHELIN 1901 Clypeaster crassicostatus, AIRAGHI, p.35,
in the base of formation verifies the age Pl.II/5, IV/1
of Middle and Upper Oligocene in these 1958 Clypeaster scillae, SMEDILE, p.35,
sediments. Pl.III/3
• The recognized genus in this formation 1966 Clypeaster scillae, MOORE, p.462
represents warm waters. 1984 Clypeaster scillae, DEMARCQ, Pl.XII/1
• The most important and abundant echinoderms Material - 9 Samples
are Scutella and Clypeaster belonging to Distribution - Miocene inferior of almost all
the coastal regions and their morphologies studied profiles.
indicate energetic environments.
• As mentioned in the A member, especially for Clypeaster aff. folium MICHELIN
the upper sandstones and the C1 submember, Pl.3, fig.2
there are layers containing echinoderms. 1859 Clypeaster folium MICHELIN, Pl.XX/2
This concentration may relate to storms and 1915 Clypeaster martini COTTREAU, p.98,
turbulence in the sea bed. Pl.XI/1-4
• Occasionally and concurrent with the 1920 Clypeaster marginatus FORTEAU, Vol.2؛
formation of layers of Scutella, the content 1958 Clypeaster folium, SMEDILE, p.32,
of glauconite increased in the sandstones. Pl.XI/3
This event corresponds to an increase of the Material - 1 Sample
depth of the sea and illustrates a transgressive Distribution - Oligocene of Dochah
case. In the upper part (B Member), the
sediments changed to sandy marls containing Clypeaster biarritzensis COTT. var. trotteri
planktonic foraminifers and glauconite as a GREGORY
result of the transgression. Pl.6, fig.2
• Their abundance of echinoderms and 1891 Clypeaster biarritzensis COTTEAU, II,
variation decreased in upper parts of the p.229
formation. This could be attributed to higher 1911 Clypeaster var. trotteri
temperature in the upper Burdigalian, GREGORY. p.662, Pl.XLVII/1
resulting in their migration from Central 1913 Clypeaster biarritzensis var. trotteri,
• After the sudden drop of temperature in the 1921 Clypeaster var. trotteri,
Lower Oligocene, the global temperature STEFAN. p.126, Pl.XVII/7
began to increase. The Burdigalian had a Material - 1 Sample
warm climate and the temperature increased Distribution - Oligocene of Shurab.
even further in the upper Burdigalian.

64Khaksar and Maghfouri, ESRJ Vol. 11, No. 1. June 2007
Suborder Scutellina 1890 Echinolampas vilanovae COTTEAU, p.73,
Superfamily Scutellidea Pl.IX/1-5
Family Scutellidae 1981 cfr. vilanovae, KALANTARI,
Genus Scutella LAMARCK, 1816 Pl.63/1-2
Scutella subrotundus (LESKE) Material - 14 Samples
Pl.2, fig.1 Distribution - Burdigalian the Kamar Kuh,
1841 Echinodiscus subrotundus LESKE (1778) Navab, Eidajti, Bichareh.
en AGASSIZ, p.5
1917 ? Lambertiella CHECCHIA- RISPOLI, Echinolampas (Macrolampas) discus DESOR
p.57 Pl.5, fig.1
1966 Scutella subrotunda, MOORE, p.477, 1858 Echinolampas discus DESOR, Synopsis,
fig.366/1 p.307
1981 Scutella subrotunda, KALANTARI, 1877 discus, DAMES, Echiniden.
Pl.61/1-4 p.43, Pl.III/1
Material - 9 Samples 1919 Echinolampas discus, STEFANINI, II,
Distribution - Oligocene and Miocene inferior of p.17
almost all the profiles. 1935 (Macrolampas) discus,
VENZO, p.230, Pl.XIX/2,3
Family Astriclypeidae Material - 8 Samples
Genus Echinodiscus LESKE, 1778 Distribution - Miocene inferior of the central
Echinodiscus balestrai OPPENH part of the basin.
Pl.3, fig.3
1939 Echinodiscus balestrai, STEFANINI, Superorder Echinacea
p.127 Order Echinoida
Material - 2 Samples Family Echinidae
Distribution - Oligocene of Bichareh and Genus Psammechinus AGASSIZ y DESOR,
Dochah. 1846
Psammechinus affinis FUCHS
Genus Amphiope AGASSIZ, 1840 Pl.7, fig.2
Amphiope bioculata (DESMOULINS) 1972 Psammechinus affinis, NAINI. p.223,
Pl.3, fig.4 fig.77,78
1815 Scutella bifora var.3 LAMARCK, p.10, 1981 affinis, KALANTARI,
n7؛ Pl.63/3-5
1837 Scutella bioculata var. A tipus Material - 3 Samples
DESMOULINS, p.232, n23؛ Distribution - Burdigalian of Shurab and
1906 Amphiope bioculata, LAMBERT, p.50 Bichareh.
1948 Amphiope bioculata, MORTENSEN,
p.413, fig.243 Order Phymosomatoida
1966 Amphiope bioculata, MOORE, p.489, Family Phymosomatidae
fig.374/1 Genus Micropsis COTTEAU, 1856
1983 Amphiope bioculato, LIOMPART, p.70, Micropsis aff. tremadesi COTTEAU
Pl.1-3 Pl.7, fig.3
Material - 1 Sample 1890 Micropsis tremadesi COTTEAU, p.96,
Distribution - Burdigalian of Eidajti. Pl.XV/3-6
Material - 2 Samples
Superorder Atelostomata Distribution - Aquitanian of Eidajti and Shurab.
Order Cassiduloida
Family Echinolampadidae Superorder Atelostomata
Genus Echinolampas GRAY, 1825 Order Spatangoida
Echinolampas cfr. vilanovae COTTEAU Suborder Micrasterina
Pl.4, fig.1 Family Spatangidae

65Paleontological study of the Echinoderms in the Qom Formation
(Central Iran)
Genus Spatangus GRAY, 1825 1951 Lovenia (Sarsella) sulcata, MORTENSEN,
Spatangus corsicus DESOR p.95, fig.44/a
Pl.7, fig.1 1966 Lovenia (Vascoaster) sulcatus, MOORE,
p.613, fig.498/3
1869 Spatangus corsicus, TARAMELLI, p.2176, Material - 4 Samples
Pl.IX/1-2 Distribution - Burdigalian of Do Baradar and
1877 Spatangus corsicus, COTTEAU in Nardaghi.
LOCARD. p.333, fig.1-3
1885 Spatangus hemiornatus MAZZETTI y Suborder Hemiasterina
PANTANELLI, p.62, Pl.I/3 Family Schizasteridae
1901 Spatangus corsicus, AIRAGHI. p.215 Genus Schizaster AGASSIZ, 1836
1919 Spatangus corsicus, STEFANINI. p.139, Schizaster cfr. beloutschistanensis D`ARCHIAC
Pl.XIV/6 y HAIME (1853)
1967 Spatangus corsicus, MENESINI, p.153, Pl.6, fig.1
Pl.II/6 1981 Schizaster cfr. beloutschistanensis,
Material - 4 Samples KALANTARI, Pl.65/13-15
Distribution - Burdigalian of Nardaghi. Material - 12 Samples
Distribution - Burdigalian of Nardaghi, Navab,
Genus Maretia GRAY, 1855 Bichareh.
Maretia aff. aragonensis COTTEAU
Pl.4, fig.2 Schizaster aff. vilanovae COTTEAU
1988 Maretia aragonensis, GOMEZ, p.640, Pl.5, fig.2
Pl.31/6 1890 Schizaster vilanovae COTTEAU, p.38,
Material - 2 Samples Pl.IV/10-13
Distribution - Miocene inferior of Bichareh and Material - 8 Samples
Do Baradar. Distribution - Aquitanian of Do Baradar,
Nardaghi, Bichareh and Jorabad.
Suborder Micrasterina
Family Loveniidae Subclass Cidaroidea
Genus Breynia DESOR, 1847 Order Cidaroida
Breynia aff. australasiae (LEACH) Family Cidaridae
Pl.8, fig.2 Genus Prionocidaris AGASSIZ, 1863
1815 Spatangus australasiae, LEACH, p.68, Prionocidaris sismondai (MAYER)
Pl.82 Pl.6, fig.3
1858 Breynia crux-andra, DESOR, p.408 1907-8 Prionocidaris sismondai MAYER, v.34,
1891 Breynia australasiae, RAMSAY, ll, p.142
p.37,55 1966 sismondai, MOORE, p, 330,
1951 Breynia australasiae, REITZEL, p.63 fig.247/1h
1946 Breynia australasiae, CLARK, p.381 Material - 1 unit (incomplete).
1951 Breynia australasiae, MORTENSEN, ll, Distribution - Burdigalian of Jorabad.
p.132, Pl.X,XI,XII
1966 Breynia MOORE, p.613, PLATES
Material - 3 Samples Plate 1
Distribution - Aquitanian of Do Baradar, Kamar 1- Clypeaster aff. scillae DESMOULINS.
Kuh and Bichareh. Aquitanian, Do Baradar. C1.2. 1a: apical view.
1b: ventral view 1c: lateral view.
Genus Lovenia (Vascoaster) LAMBERT, 1915
Lovenia (Vascoaster) sulcatus (HAIME) Plate 2
Pl.8, fig.1 1- Scutella subrotundus (LESKE). Aquitanian,
1853 Breynia sulcatus HAIME, p.216 Do Baradar. 3a: C1.8, apical view 3b: C1.11,