Department of Physics and Geology University of Perugia
Pars Geological Research Center ARIANZAMIN
ABSTRACTBOOK
SCIENTIFICANDORGANIZINGCOORDINATORSRobertoRettoriMansourGhorbaniORGANIZINGCOMMITTEERobertoRettori(UniversityofPerugia,Italy)SimonettaCirilli(UniversityofPerugia,Italy)CaterinaPetrillo(UniversityofPerugia,Italy)MansourGhorbani(Arianzamin,Iran)EnricoCapezzuoli(UniversityofPerugia,Italy)MarcoCherin(UniversityofPerugia,Italy)AmaliaSpina(UniversityofPerugia,Italy)LuciaAngiolini(UniversityofMilano,Italy)AnoshiravanKani(Arianzamin,Iran)SCIENTIFICCOMMITTEEDemirAltiner(MiddleEastTechnicalUniversity,Ankara,Turkey)MarcoBalini(UniversityofMilano,Italy)SvevaCorrado(UniversityofRomaTre,Italy)JalilGhalamghash(GeologicalSurveyofIran)HormozGhalavand(NIOC,Iran)BahaeddinHamdi(Arianzamin,Iran)RossanaMartini(UniversityofGeneva,Switzerland)ShuzhongShen(NanjingInstituteofGeologyandPaleontology,China)BahmanSoleimany(NIOC,Iran)MichaelStephenson(BritishGeologicalSurvey)AlirezaTahmasebi(NIOC,Iran)AndreaZanchi(UniversityofMilanoBicocca,Italy)
1
Good morning Ladies and Gentlemen,
I welcome all the distinguished scientists, researchers and participants in
this congress. I would like to thank Professor Roberto Rettori and his
colleagues at Perugia University, especially Dr. Amalia Spina, for all their
efforts in convening this Congress. I also wish to thank my colleagues at
Arian Zamin Research Centre in Iran, Dr. Anoushiravan Kani, Dr. Hamdi,
Dr. Ahifar, Mr. Zand and Ms. Aftabi.
I wish to thank the Department of Physics and Geology (University of
Perugia), NIOC, Geological survey of Iran, Società Geologica Italiana,
Società Paleontologica Italiana, Department of Earth Science “A.Desio”
(University of Milan) and Professor Lucia Angiolini, CIMP –
“Commission Internationale Microflore Paléozoïque”, IntGeoMod and
Esanda.
Arian Zamin and the University of Perugia were the proponents of this
event and Arian Zamin has pledged all the financial supports.
This congress, apart from its scientific objectives, is the beginning of a
joint scientific work, at an international level, that Perugia University and
Arian Zamin have undertaken.
The history of scientific and cultural cooperation between Italy and Iran
is very long and in fact it dates back to many centuries which, in turn,
refers to the antiquity of the two countries.
In the past the European culture reached Iran and the East via the ancient
Rome, and the Eastern culture reached Europe through ancient Iran which
was a major part of the Asia.
There have been trades and exchange of culture and friendship between
the two nations for thousands of years. Italians were engaged in teaching at
the University of Jondishapoor (present-day Ahwaz) in Sasanid era. In
Safavid era, Shah Abbas had a very good relationship with Venetian
Government and the first trade agreement between the two countries was
signed in Sarvenia town.
2
In Pahlavi era many cultural heritages and buildings, in Iran, were
repaired and strengthened by Italian company. Italian companies also were
involved in establishing industrial factories in Iran.
Following the Iranian Nuclear deal, the Iranian President, Dr. Hassan
Rouhani, visited Italy first, on his European tour. At present, there is a
strong cultural relationship between the two nations.
The two nations have a lot in common. Respecting all the values each
person has, message of friendship and peace for everybody and different
nations, irrespective of their race, gender, beliefs and geography are a few
to mention.
I hope this congress will be the first step stone for future scientific and
cultural cooperation between Iran and the rest of the world and also paves
the way for geo-tourism in Iran.
I would like to thank you all for attending this congress.
Thank you.
Mansour Ghorbani
Managing Director of Arian Zamin Geological Research Center and
Associate Professor at Shahid Beheshti University
3
Summary
INNOVATION COLLABORATION; NEW MISSION OF R&T DIRECTORATE OF NIOC - Alavi Taleghani E. ..... 7
ULTIMATE MORPHOLOGICAL CHANGES BEFORE THE END-PERMIAN EXTINCTION: CHANGHSINGIAN
SMALLER FORAMINIFERA FROM THE SOUTHERN BIOFACIES BELT IN TURKEY - Altiner D., Özkan-
Altiner S., Şahin N., Atasoy S.G. ..................................................................................................................................... 8
UPPER PERMIAN BRACHIOPODS FROM NORTHERN IRAN: THEIR VALUE FOR CORRELATIONS AND
FOR UNDERSTANDING THE END PERMIAN MASS EXTINCTION - Angiolini L., Garbelli C., Bahrammanesh
Tehrani M. ......................................................................................................................................................................... 9
PALYNOSTRATIGRAPHY OF CARBONIFEROUS STRATA IN SOUTHEAST TABAS, CENTRAL IRAN BASIN
- Aria-Nasab M., Spina A., Daneshian J. ......................................................................................................................... 10
EVIDENCES OF MAJOR LOWER PALAEOZOIC DISCONTINUITY IN KUH-E GAHKUM IN THE BANDAR
ABBAS AREA (ZAGROS, IRAN) - Asghari A., Vennin E., Soleimany B., Hajian M., Hasan Goodarzi M., Alavi
Taleghani E. ..................................................................................................................................................................... 11
SEQUENCE-STRATIGRAPHY AND TECTONO-STRATIGRAPHY OF PERMIAN SUCCESSION IN THE
CENTRAL ALBORZ (NESEN AREA) - Asilian Mahabadi H., Farahani M., Saeidi A. ............................................... 12
THE FIRST RECORD OF CAMBRIAN CONODONTS FROM THE HUQF-HAUSHI OUTCROPS, SULTANATE
OF OMAN, ARABIAN PENINSULA - Bagnoli G., Machado G., Marjibi S. ............................................................... 13
BIOSTRATIGRAPHY AND PALEOECOLOGY OF CARBONIFEROUS BRACHIOPODS FROM NW TAR LAKE
(DAMAVAND, N IRAN) - Bahrammanesh Tehrani M. ................................................................................................. 14
FIRST REPORT OF LATE PENNSYLVANIAN AMMONOIDS AND CISURALIAN CONODONTS FROM
CENTRAL IRAN: STRATIGRAPHIC SETTING AND PALAEOBIOGEOGRAPHIC SIGNIFICANCE IN THE
FRAMEWORK OF THE GONDWANAN GLACIATIONS - Balini M., Mandrioli R., Nicora A., Angiolini L.,
Borlenghi L.M., Vuolo I., Sohrabi Z., Bahramanesh Tehrani M. .................................................................................... 15
RECONSTRUCTIONS OF THE CENTRAL TETHYS DOMAIN SINCE THE MIDDLE PERMIAN: THE DARIUS
PALAEOTECTONIC MAPS - Barrier E., Vrielynck B., Robertson A., Zanchi A., Brouillet J.F. .................................. 16
THE PERMIAN STRATIGRAPHY OF HAZRO (GONDWANA MARGIN OF SE TURKEY): FROM FLUVIO-
DELTAIC TO CARBONATE RAMP ENVIRONMENTS, NEW DATA - Baud A., Angiolini L., Broutin J., Crasquin
S., Gaillot J., Vachard D. ................................................................................................................................................. 17
END-PALEOZOIC EVENTS ON OMAN AND INDIAN GONDWANA MARGIN
- Baud A., Richoz S., Krystyn L ....................................................................................................................................... 18
LATE PALAEOZOIC TERRESTRIAL VERTEBRATE FAUNA: A GLOBAL VIEW FROM AN ITALIAN
PERSPECTIVE - Bernardi M., Petti F.M. ....................................................................................................................... 19
STRATIGRAPHIC EVIDENCE OF THE LATE PALAEOZOIC ACTIVE MARGIN IN NE IRAN: CONSTRAINTS
ON THE RECONSTRUCTION OF THE NORTHER SIDE OF THE PALAEOTETHYS - Berra F., Zanchetta S.,
Zanchi A., Bergomi M., Nicora A., Heidarzadeh G. ....................................................................................................... 20
A CHRONOSTRATIGRAPHIC FRAMEWORK FOR THE CARBONIFEROUS KASHAGAN BUILDUP, PRE-
CASPIAN BASIN, KAZAKHSTAN - Brenckle P.L., Collins J.F. ................................................................................. 21
FIRST RECORD OF CRYPTOSPORES IN POST-HIRNANTIAN (LATEST ORDOVICIAN-EARLY SILURIAN)
SEDIMENTS FROM ETHIOPIA - Brocke R., Bussert R., Steemans P. ........................................................................ 22
PHYTO- AND PALAEOGEOGRAPHIC IMPLICATIONS OF MISSISSIPPIAN MIOSPORE ASSEMBLAGES
FROM SAUDI ARABIA - Clayton G., Breuer P., Hooker N. ........................................................................................ 23
4
BIOSTRATIGRAPHIC INVESTIGATION OF THE MILA FORMATION ALONG THE SHAHMIRZAD SECTION,
NORTH OF SEMNAN WITH SPECIAL REFERENCE TO CONODONTS - Fazli L., Rezaiparto K. ........................ 24
AN OVERVIEW OF DEVONIAN TO PERMIAN IN ALBORZ MOUNTAINS, NORTH IRAN - Gaetani M. .......... 25
MIDDLE-LATE PERMIAN BIOSTRATIGRAPHY (ALGAE AND FORAMINIFERS) OF THE HAZRO SECTION
(SOUTHEASTERN TURKEY) - Gaillot J., Vachard D., Baud A. ................................................................................. 27
PRELIMINARY DISCUSSION ON PERMIAN FORAMINIFERAL ASSEMBLAGES IN NW AND CENTRAL
IRAN - Gennari V., Rettori R., Angiolini L., Ghorbani M. ............................................................................................. 28
PALAEOZOIC GRANITOID IN IRANIAN PART OF GONDWANALAND - Ghalamghash J. ................................ 29
FUSULINIDS FROM LATE CARBONIFEROUS AND EARLY PERMIAN OF COLOMBIA - Gómez Cruz A.,
Moreno-Sánchez M., Lemus-Restrepo A., Vachard D. ................................................................................................... 30
CONODONT COLOR ALTERATION MAPS FOR PALAEOZOIC TO EARLY TRIASSIC DEPOSITS OF THE
ALBORZ MTS - Haghighat N., Hamdi B. . ..................................................................................................................... 31
CLIMATOSTRATIGRAPHY OF THE CARBONIFEROUS–PERMIAN IN THE EAST GONDWANA INTERIOR
RIFT - Haig D.W., Mory A.J. .......................................................................................................................................... 32
CHARACTERIZATION OF THE MAJOR UNCONFORMITIES OBSERVED IN PRE-KHUFF PALAEOZOIC
SUCCESSION OF THE KUH-E SURMEH (FARS AREA), KUH-E FARAGHAN AND KUH-E GAHKUM
(BANDAR ABBAS AREA) IN SOUTH OF IRAN - Hasan Goodarzi M.G., Asghari A., Vennin E., Soleimany B.,
Hajian M. ......................................................................................................................................................................... 33
MIOSPORE ASSEMBLAGES FROM PŘÍDOLÍAN TO EARLY EIFELIAN SEQUENCES OF THE OUED
SAOURA ALGERIAN SAHARA - Hassan Kermandji A.M., Khelifi Touhami F. ....................................................... 34
NEW DATA ON THE PALYNOLOGY OF THE DEVONIAN AND CARBONIFEROUS OF NW-AFRICA
(ALGERIA, MAROCCO) - Jäger H. .............................................................................................................................. 35
OPTICAL KEROGEN ANALYSIS FOR ENHANCED ANALYSIS OF HYDROCARBON SYSTEMS: FROM
MATURE EUROPEAN BASINS TO NEW EXPLORATION IN NORTHERN GONDWANA - Jäger H. ................. 36
LATE PRECAMBRIAN-EARLY PALEOZOIC STRATIGRAPHY OF NORTHERN GONDWANA REGION WITH
SPECIAL EMPHASIS ON IRAN - Kani A., Ghorbani M. ............................................................................................. 37
A SUMMARY OF THE CURRENT INVESTIGATIONS ON PALAEOZOIC ROCKS OF IRAN -
Kani A., Ghorbani M. ...................................................................................................................................................... 38
THE CONTINUITY OF RIFTING PHASE AND ITS IMPACT ON HYDROCARBON DISTRIBUTION DURING
THE CARPITANIAN IN THE FARS PLATFORM OF THE ZAGROS FOLD BELT, SW IRAN - Kavoosi M.A. .... 39
EXTENSIONAL MOVEMENTS DURING THE EARLY MIDDLE CAMBRIAN RECORDED IN THE MEMBER 1
OF MILA FORMATION IN THE EASTERN ALBORZ MOUNTAIN RANGE - Kavoosi M.A., Shamani F. ........... 40
LATE DEVONIAN ORGANIC-WALLED MICROPLANKTON FROM CENTRAL PORTUGAL AND ITS
IMPLICATIONS ON PALEOGEOGRAPHY - Machado G., Vavrdova M. .................................................................. 41
SEQUENCE STRATIGRAPHY OF THE PERMIAN-TRIASSIC BOUNDARY IN THE CENTRAL PERSIAN GULF:
NEW INSIGHTS FROM A NOVEL AND INTEGRATED APPROACHES - Mazaheri Johari M., Moradi M.,
Bahrammanesh Tehrani M., Eidani M. ............................................................................................................................ 42
APPLICATION OF THE SOFTWARE TSC TO DEPICT GLOBAL SEA-LEVEL CHANGES AND SEQUENCES -
Moezzi Nasab R., Mohamadi M. ..................................................................................................................................... 43
EARLY PALEOZOIC THICKNESS VARIATION CONTROL ON DEFORMATION STYLE IN THE CENTRAL
5
FARS: IMPLICATIONS FOR HYDROCARBON RXPLORATION - Motamedi H. ................................................... 44
SHANITA ZONE WITHIN THE MIDDLE-UPPER PERMIAN CHRONOSTRATIGRAPHIC FRAME IN TURKEY -
Özkan-Altiner S., Altıner D., Şahin N. ............................................................................................................................ 45
GEOCHEMISTRY OF IRONOXIDE, APATITE AND REE ELEMENTS FROM LACKE-SIAH, BAFGH
(CENTRAL IRAN) - Pur Nourbakhsh F., Lotfi M., Rezaie Rad A. ................................................................................ 46
A TRANSITION FROM PRE-RIFT AND POST-RIFT SEQUENCES IN THE ZAGROS REGION AND CENTRAL
IRAN - Piryaei A. ........................................................................................................................................................... 47
CHARACTERIZATION AND SOURCE ROCK POTENTIAL OF PALAEOZOIC SEQUENCE IN THE ZAGROS
BASIN, IRAN - Rashidi M., Solimany B., Tahmasebi Sarvestani A., Daryabandeh M., Hajian M. .............................. 48
HYDROCARBON POTENTIAL AND KEROGEN STRUCTURE EVALUATION OF PERMIAN FARAGHAN
FORMATION IN ZAGROS BASIN OF IRAN - Rashidi M., Tsuchida K., Daryabandeh M., Ghorbani M. ................ 49
COLD TEMPERATE BIOTAS AND GLACIAL CONDITIONS DURING THE LATE PALEOZOIC ICE AGE
(LPIA): NEW TIMING AND BETTER TEMPERATURES - Runnegar B., Beard A., Ivany L. .................................. 50
LATE DEVONIAN AND EARLY CARBONIFEROUS MIOSPORES AND ACRITARCHS FROM THE
SOUTHERN TABAS BLOCK (ZARAND REGION), CENTRAL IRAN - Sabbaghiyan H., Aria-Nasab M. .............. 51
STABLE SULFUR ISOTOPE VARIATION AND FLUID INCLUSION STUDIES FROM EPITHERMAL PYRITE –
GALENA VEINS AT SPOOHK AREA (KABUTAR KUH) SE GONABAD, EAST IRAN - Sadeghi L. ................... 52
CONTRIBUTION TO THE EVOLUTION OF THE NORTHERN GONDWANA MARGIN IN TURKEY:
GEODYNAMIC SIGNIFICANCE OF THE MIDDLE PERMIAN TO LOWER TRIASSIC SUCCESSIONS IN THE
ANTALYA NAPPES (WESTERN AND CENTRAL TAURIDES) - Şahin N., Altiner D. ........................................... 53
THERMAL EVOLUTION OF THE HOLY CROSS MOUNTAINS (CENTRAL POLAND) THROUGH
MODELLING OF NEW AND OLD THERMAL MATURITY INDICATORS OF PALAEOZOIC SEDIMENTARY
SUCCESSIONS - Schito A., Corrado S., Trolese M., Aldega L., Caricchi C., Cirilli S., Spina A. ................................ 54
NEW RAMAN PARAMETERS INTEGRATED IN CLASSICAL PETROLEUM SYSTEM MODELLING TO
ASSESS THERMAL EVOLUTION OF SEDIMENTARY BASINS: FOUR CASE HISTORIES FROM CENOZOIC,
MESOZOIC AND PALEOZOIC SEDIMENTARY SUCCESSIONS - Schito A., Corrado S., Romano C., Guedes A.,
Grigo D. ........................................................................................................................................................................... 55
LOWER PALEOZOIC PALY IN ZAGROS, PROSPECTIVITY AND CHALLENGES - Soleimany B. ..................... 56
APPLICATION OF PALYNOMORPH DARKNESS INDEX (PDI) AND MICROSPECTROSCOPY TO ASSESS
THERMAL MATURITY AND ASSOCIATED CHANGES IN CHEMISTRY OF PALYNOMORPHS: A CASE
STUDY FROM NORTH AFRICA - Spina A., Marcogiuseppe A., Cirilli S., Rettori R., Di Michele A., Sassi P., Vecoli
M., Riboulleau A., Servais T. . ......................................................................................................................................... 57
GONDWANAN PALAEOZOIC PLANT SPORES: A REVIEW - Steemans P., Gerrienne P. ..................................... 58
PERMIAN PALYNOSTRATIGRAPHY: PROGRESS AND CHALLENGES FOR THE NEXT CENTURY -
Stephenson M. ................................................................................................................................................................. 59
PALYNOLOGICAL ASSEMBLAGES ACROSS THE HERCYNIAN UNCONFORMITY IN WESTERN IRAQ -
Stephenson M., Al-Mashaikie S. ..................................................................................................................................... 60
SELECTED SPORES AND POLLEN FROM THE PERMIAN UMM IRNA FORMATION, JORDAN, AND THEIR
STRATIGRAPHIC UTILITY IN THE MIDDLE EAST AND NORTH AFRICA - Stephenson M., Powell J. ............ 61
NEW TAXONOMICAL AND PALAEOGEOGRAPICAL DATA OF SMALLER TETHYAN FORAMINIFERS -
Vachard D. ....................................................................................................................................................................... 62
6
ANGELITA (FORAMINIFERA, PSEUDOVIDALINIDAE), AS A MARKER OF THE OPENING OF NEOTETHYS
DURING THE MIDDLE-LATE PERMIAN - Vachard D., Rettori R., Altıner D., Gennari V., Grigoryan G.,
Zambetakkis A., Ghazzay W., Razgallah S., Ghorbani M., Kani A., Aria-Nasab M., Sabbaghian H., Keyvan Z. ......... 63
EARLY TRIASSIC FAUNA (MAINLY FORAMINIFERS) FROM CAUCASUS AND GORNY MANGYSHLAK -
Vuks V. J. ........................................................................................................................................................................ 64
7
INNOVATION COLLABORATION; NEW MISSION OF R&T
DIRECTORATE OF NIOC
Alavi Taleghani E.
Iran has about 160 Billion barrels of oil as proved reserves and 34TCM of gas. National Iranian Oil
Company (NIOC) produced 3.15 million barrels of oil and 550 MCM of gas daily on 2015.
Because of long history (more than 100 years) of producing of oil and gas by NIOC and due to
characteristics of Iran's reservoirs, NIOC has defined 11 different technological target areas such as:
IOR/EOR, production optimization, reservoir management, earth sciences, drilling and so on
Hereupon IOR/EOR is one of the most priority targets.
For achieving IOR/EOR expectations, NIOC has signed different contracts with Iranian universities
and has dedicated 20 big oil and gas fields including 52 reservoirs to those universities for 10 years.
But there are two obligations for universities. First they have to have at least one foreign university
as joint venture and second they have to deliver a technological road map for each special field and
thus upcoming projects would be on the basis of that road map.
One of the main goals of this contracts and jointing venture with international companies and
universities are transferring of technology and innovation collaboration. These would be basis for
cooperation between NIIOC and Iranian and international universities and companies through all
value chain of oil industry in upstream from exploration to development and production.
STI and DUI innovation modes are one of the main tasks for R&T directorate of NIOC in
cooperating with national and international universities and companies to improving and
transferring of technology and also innovation collaboration especially in IOR/EOR issue. In this
relation we welcome any joint projects with Iranian universities that provide us the above
mentioned targets.
8
ULTIMATE MORPHOLOGICAL CHANGES BEFORE THE END-PERMIAN
EXTINCTION: CHANGHSINGIAN SMALLER FORAMINIFERA FROM
THE SOUTHERN BIOFACIES BELT IN TURKEY
Altiner D., Özkan-Altiner S., Şahin N., Atasoy S.G.
The Changhsingian of the Southern Biofacies Belt in Turkey is widely distributed in the Arabian
Platform and in the Geyik Dagi and Aladag tectonic units and the Antalya Nappes of the Anatolide-
Tauride Block. From non-fusulinoidean Fusulinata two distinct evolutionary trends, both belonging
to the family Globivalvulinidae, occur in the Changhsingian. In the globivalvulinin trend,
Paraglobivalvulina originated from Globivalvulina vonderschmitti close to the Capitanian-
Wuchiapingian boundary commonly occurs in the latest Permian. Among the other descendants in
this stock, Charliella, seems to have gone extinct at the Wuchiapingian-Changhsingian boundary
and Urushtenella derived from Paraglobivalvulina occurs rarely in the Changhsingian. From the
Septoglobivalvulina-Paraglobivalvulinoides lineage Paraglobivalvulinoides is rather rare and
sporadic. One of the most remarkable evolutionary trends in the Southern Biofacies Belt is in the
dagmaritin-type globivalvulinids. Paradagmarita, derived from Crescentia very close to the
Wuchiapingian-Changhsingian boundary, comprises three distinct species (P. monodi, P.
flabelliformis, P. planispiralis) in the Changhsingian. A new genus originated from Paradagmarita
in the younger levels of the Changhsingian is characterized by a hook-shaped apertural flap
protecting partly the apertural system. In addition, Paradagmacrusta derived from Paradagmarita
close to the Wuchiapingian-Changhsingian boundary and Louisettita originated from Dagmarita in
the late Wuchiapingian commonly occur in the Changhsingian.
In the Southern Biofacies Belt, although Nodosariata occurs abundantly, colaniellids are totally
absent. Syzraniidae, Protonodosariidae, Geinitzinidae, Robuloididae, Frondinidae and
Pachyphloiidae frequently occur. From robuloidids, the genus Robuloides is frequent and displays
distinct morphological variations close to the Permian-Triassic boundary.
Several genera belonging to Miliolata, such as Agathammina, Hemigordius, Midiella, Neodiscus,
Multidiscus, Neodiscopsis and Glomomidiellopsis occur rarely to commonly in the Changhsingian
of the Southern Biofacies Belt. Among these taxa, distinct evolutionary changes occurred in the
populations of Glomomidiellopsis (G. uenoi, G. lysitiformis). The genus Kamurana s.s. was
probably derived from Glomomidiellopsis in the late Changhsingian.
9
UPPER PERMIAN BRACHIOPODS FROM NORTHERN IRAN: THEIR
VALUE FOR CORRELATIONS AND FOR UNDERSTANDING THE END
PERMIAN MASS EXTINCTION
Angiolini L., Garbelli C., Bahrammanesh Tehrani M.
The Upper Permian successions of North Iran have been known for a long time to be among the
most fossiliferous of the Neotethys-Palaeotehys shores (Angiolini & Carabelli, 2010; Ghaderi et al.,
2014; Garbelli et al 2014; and references therein). The dominant benthic fauna preserved in these
successions is that of brachiopods, which are thus very important in discussions of Late Permian
correlations, and to unravel the dramatic faunal turnover of marine organisms at the end of the
Palaeozoic.
Here, we revise the Upper Permian brachiopod biozonation of the Permian successions of the Ali
Bashi Mountains, NW Iran and of the Alborz Mountains, N Iran, and discuss both their mutual
correlations, which is not without issues, and their correlation to the less diversified faunas of
Central Iran, where only few wide-ranging species seem to occur. Correlations with South China
are also tempted, even if made difficult by the extreme diversity of the Chinese fauna; they show
common generic occurrences mostly in the Changhsingian.
Also, we discuss the brachiopod distribution pattern and its causes at the end of Permian, a pattern
which is different in N Iran with respect to NW Iran. In the successions of the Alborz Mountains,
the brachiopod fauna disappears about twenty metres below the Permian/Triassic boundary, as also
recorded in other localities of the western Tethys (Angiolini et al., 2010). In contrast, in the Ali
Bashi Mountains successions, a few brachiopods range higher, in the end-Permian extinction
interval, as recorded in many sections of South China. They thus provide a key to understand the
latest Permian events.
10
PALYNOSTRATIGRAPHY OF CARBONIFEROUS STRATA IN
SOUTHEAST TABAS, CENTRAL IRAN BASIN
Aria-Nasab M., Spina A., Daneshian J.
The well preserved palynomorphs of Shishtu-II rock unit with a thickness of 303 m in Howz-e-
Dorah area located in the southeast Tabas, Central Iran Basin - indicate a Tournaisian - Visean age
for this rock unit. The main lithology of Shishtu-II consists of shale, sandstone, dolomite and
limestone. Investigation of palynomorphs distribution led us to recognize three palynological
biozones based on appearance and disappearance of spores, including PC, CM and Mag. These
biozones are comparable with European and South American continents. This study shows a hiatus
between Shishtu-I and II rock units, and the Mush Horizon which in previous works had been
considered as uppermost Shishtu-I, in fact, belongs to Shishtu - II. The presence of few acritarchs
such as Veryhachium spp., Stellinium sp. and Gorgonisphaeridium sp. mention to very near shore
environment for this rock unit. On the other hand, existence of spores such as Indotriradites
dolianitii and I. daemoni indicates relation of this area to the Gondwana Continent.
11
EVIDENCES OF MAJOR LOWER PALAEOZOIC DISCONTINUITY IN
KUH-E GAHKUM IN THE BANDAR ABBAS AREA (ZAGROS, IRAN)
Asghari A., Vennin E., Soleimany B., Hajian M., Hasan Goodarzi M.,
Alavi Taleghani E.
In the Arabian plate and the Zagros area, the Palaeozoic deposits are important Petroleum system
with Silurian shales considered as hydrocarbon source rocks and Ordovician, Devonian and Lower
Permian sandstones and dolomites recognized as good reservoirs locally. Evidences for major
unconformity in the Lower Palaeozoic succession in Zagros lead to question the role of
tectonic/eustatism/climate on their formation. The Palaeozoic succession of Kuh-e Gahkum
Anticline is characterized by the preservation of thin Cambrian, Silurian, Devonian and Lower
Permian Formations separated by a large hiatuses. The first unconformity in the Lower Palaeozoic
present in Kuh-e Gahkum, encompassing from the Combrian up to the Lowermost Silurian. The
Silurian succession corresponds to five depositional environments evolving from proximal to distal
platform: (1) Fan delta; (2) Lagoon; (3) Shoreface; (4) Upper offshore; and (5) Deep offshore
environments. The local erosion of the Seyahou Formation, observed in the neighbouring areas
closed to the Kuh-e Gahcum anticline (i.e. Kuh-e Faraghan) allows the precise the role of the
different controlling factors. In Kuh-e Faraghan, the Silurian deposits correspond to lower up to
upper offshore. These mainly clastic successions represent good source rocks and reservoirs in the
regional Palaeozoic Petroleum system of the Zagros area separated by a major unconformity. The
influence of regional tectonism and climate related to the late Ordovician glaciations cannot be
ruled out from possible candidate participating to erosion, but a local diapir doming seems to better
explain part of this local intense erosion.
12
SEQUENCE-STRATIGRAPHY AND TECTONO-STRATIGRAPHY OF
PERMIAN SUCCESSION IN THE CENTRAL ALBORZ (NESEN AREA)
Asilian Mahabadi H., Farahani M., Saeidi A.
The Alborz mountain range, which located in northpart of Iran, separates the south Caspian, (in the
north) from the central Iranian Basin (in the south). The Alborz mountain with about 2000 km
length extends from Azarbaijan boundary to the Afghnistan. The Permian sequence is well exposed
in Nesen area, about south-eastern Caspian sea. The Paleozoic sediments with Gondwanian affinity
has been folded in both Cimmerian and Alpine orogenesis. In this range the Permian rocks
deposited in a new-developed basin during drifting of Iranian block. The Permian sequence has
been divided into the Dorud Formation (early Permian), Ruteh Formation (middl-late Permian) and
Nesen Formations (late Permian). The Permian strata disconformably lies on the Carboniferous
deposits (Mobarak Formation) and it is disconformably overlain by the Triassic strata (Elika
Formation). The Dorud Formation (Asselian-Sakmarian) mainly composed of red sandstone,
conglomerate, red-white quartzarenite and fossiliferous limestone. The Ruteh Formation
(Artinskian to Midian) is composed of massive to thick-bedded limestone. The Nesen Formation
(Dzhulfian) begins with a basaltic unit in the base and black to dark gray shale and black thin-
medium bedded limestone in the top.
Detailed field and petrographic studies were carried out and resulted in recognition of seven
petrofacies and 15 carbonate microfacies of which deposited in a mixed siliciclastic-carbonate
setting of a carbonate ramp.
Sequence stratigraphy of the Permian deposits in the study area indicate that there are nine 3rd –
order depositional sequence.
Permian deposits have recorded evidence of an extensional regime in the Alborz mountain range
inferred from the basaltic eruptions in the contact of the Ruteh and Nesen Formations.
13
THE FIRST RECORD OF CAMBRIAN CONODONTS FROM THE HUQF-
HAUSHI OUTCROPS, SULTANATE OF OMAN, ARABIAN PENINSULA
Bagnoli G., Machado G., Marjibi S.
Outcrops of the Cambrian sedimentary successions of the uppermost Miqrat Fm., the Al Bashair
Fm. and the basal Barik Fm. have been sampled for conodont and palynological investigations.
These are part of the Paleozoic Haima Supergroup, exposed in the Huqf-Haushi area in central
eastern Oman, Arabian Peninsula. The aim was to obtain two independent biostratigraphic sets of
data that can be used for correlation with the subsurface strata. Unfortunately palynology samples
were barren, but a small conodont faunule has been recorded from bioclastic and oolitic limestone
from the middle part of the Al Bashair Fm. The Al Bashair Fm. is an important regional
hydrocarbon seal and is ubiquitous in the subsurface of Central and North Oman; it reaches the
surface in the Huqf-Haushi area in central eastern Oman. The formation is composed of shales,
carbonates and siltstones deposited in a shallow marine environment and arranged in m-scale
coarsening upwards cycles. The available paleontological data for the Al Bashair Fm. includes
trilobites from the same outcrops and palynomorphs from the subsurface. The conodont faunule is
the first reported from the Cambrian of the Arabian peninsula and include Phakelodus tenuis,
Prooneotodus gallatini, Muellerodus? erectus, Nogamiconus sp., Westergaardodina sp., Furnishina
sp. The presence of Muellerodus? erectus allows the recognition of the Muellerodus? erectus Zone
established in North China (late Paibian – early Jiangshanian), in agreement with previous reports
on the trilobite fauna from the same interval.
14
BIOSTRATIGRAPHY AND PALEOECOLOGY OF CARBONIFEROUS
BRACHIOPODS FROM NW TAR LAKE (DAMAVAND, N IRAN)
Bahrammanesh Tehrani M.
This is the first study of brachiopod from the Carboniferous deposits of western Tar Lake (N Iran).
The identified taxa are classified in the Suborders Productida, Orthotetida, Orthida, Rhynchonellida,
Athyrididina, Spiriferinida and Subfamily Syringothyridinae and are Mississippian, middle-late
Tournaisian-early Visean in age. The identified brachiopod taxa are Chonetoida indet, Delepinea cf.
comoides (Sowerby, 1822), Productidae indet, Marginatia sp., Tomiproductus vaughani (Muir-
Wood, 1928), Tomiproductus elegantulus (Tolmachev, 1924), Schellwienella sp., Rhipidomella sp.,
Rossirhynchus adamantinus Gaetani, 1964, Sulcathyris cf. campomanesii (Verneuil & Archic,
1845), Spiriferidae indet, Spirifer sp., Ectochoristites sp., Paralellora sp., Unispirifer sp.,
Unispirifer (Unisiprifer) cf. striatoconvolutus (Benson & Dun & Brown, 1920), Eospiriferina sp.
and Syringothyris sp.. From a paleoecological perspective, this assemblage indicates shallow marine
conditions in a warm and humid upper Paleozoic inner ramp.
15
FIRST REPORT OF LATE PENNSYLVANIAN AMMONOIDS AND
CISURALIAN CONODONTS FROM CENTRAL IRAN:
STRATIGRAPHIC SETTING AND PALAEOBIOGEOGRAPHIC
SIGNIFICANCE IN THE FRAMEWORK OF THE GONDWANAN
GLACIATIONS
Balini M., Mandrioli R., Nicora A., Angiolini L., Borlenghi L.M.,
Vuolo I., Sohrabi Z., Bahramanesh Tehrani M.
The Late Pennsylvanian to Guadalupian sedimentary succession exposed at Bagh-e-Vang and
Shesh Angosht, south of Shirgesht and about 60 m north of Tabas (Central Iran), has been studied
in the last five years with the purpose of revising litho-, bio- and chronostratigraphy, in a framework
of a project funded by Darius Programme. The studied succession consists of Sardar and Jamal
formations, that have been sampled at 9 stratigraphic sections. Here we focus on the unconformity
between the two units.
The uppermost part of the Sardar Formation is very poor in fossils, but very few ammonoids
belonging to Agathiceras and Marathonites have been collected from two sites. The latter genus is
age diagnostic and support the attribution of the top of the Sardar Formation to the Gzhelian. This
result is unexpected, because in other sites of Central Iran, such as Zaladou and Anarak (Leven and
Gorgij, 2006a,b; Leven et al., 2006) the Gzhelian age is documented in the unit unconformably
overlying the Sardar Formation.
The lowermost part of the Bagh-e-Vang Member of the Jamal Formation has yielded some
conodont faunas and few brachiopods. The conodont fauna identified at Bagh-e- Vang consists of
Mesogondolella manifesta, M. monstra, Streptognathodus aff. lanceatus, Streptognathodus
postconstrictus, Streptognathodus postfusus and Sweetognathus aff. binodosus. These taxa support
an early Sakmarian age for the base of the unit.
A conodont fauna collected at the very base of the Bagh-e-Vang Member at Shesh Anghost is quite
younger, and includes Sweetognathus guizhouensis and transitional forms Sweetognathus whitei to
S. guizhouensis. The age of this fauna is Artinskian-Kungurian. Few small brachiopods from the
same level are assigned to Costispinifera, which suggests an Early Permian age.
According to the new data, the siliciclastic sedimentation of the Sardar Formation persisted, at least
in the studied area, until the Gzhelian. The transgression of the Bagh-e-Vang Member occurred
much before than the Yakhtashan/ Bolorian/early Murgabian age suggested by fusulinds (e.g. Leven
et al., 2007; Leven & Gorgij 2011; Partoazar et al., 2014). Its correlation with other localities of
Central Iran is discussed; the age discrepancy between Bagh-e-Vang and Shesh Angosht is
explained in term of local and strong tectonic control. The paleobiogeographic affinity of the
ammonoid faunas is notably Uralian and suggests a paleoceanographic circulation influenced by
Gondwanan glaciation.
16
RECONSTRUCTIONS OF THE CENTRAL TETHYS DOMAIN SINCE THE
MIDDLE PERMIAN: THE DARIUS PALAEOTECTONIC MAPS
Barrier E., Vrielynck B., Robertson A., Zanchi A., Brouillet J.F.
The DARIUS Programme (2010-2015) was a multi-disciplinary geological program sponsored by
Major Oil Companies and Research Organizations. The main objective was characterizing the tecto-
stratigraphic evolution since the Late Palaeozoic of a domain centered on Central Tethys extending
from Black-Sea Anatolia in the west to western Central Asia in the east. 116 original scientific
projects, executed by 150 research institutions from 25 countries, were funded by DARIUS.
Collection of original data and regional syntheses characterized the scientific activity of the
Programme. The DARIUS Programme was designed ultimately to provide new and modern insights
on the geodynamic-tectonic development of this region through a set of 20 Palaeotectonic maps
ranging in age from the Middle Permian to the Pliocene.
The maps of the DARIUS atlas are palinspastic reconstructions of the south-central Eurasian and
north African-Arabian plates starting after the Late Palaeozoic orogenies. The maps depict the
major tectonic-geodynamic features as well as the main paleofacies and paleoenvironments. Our
reconstructions are based on (1) an up-to-date kinematics reconstruction of the Africa, India and
Arabia with respect to Eurasia, and (2) an accurate timing of the tectonic events that have succeeded
since the Late Permian.
Three main periods have succeeded since the Late Palaeozoic during the subsequent opening and
closure of the Neo-Tethys oceanic domain. The first period, lasting from Permian to Liassic times,
is related to the evolution of the Cimmerian blocks (Fig.1) that successively (1) detached from the
northern margin of southern Pangea in the Early Permian, (2) drifted northward during the closure
of the Paleo-Tethys oceanic domain during the Mid-Late Permian to Triassic times, and (3) finally
collided with northern Pangea from mid-Triassic to Liassic times.
The second period is mainly characterized by the northward subduction of Neo-Tethys beneath the
southern Laurasian-Eurasian margins (Fig.2). This 140 My-long subduction (from the Jurassic to
the Early Cenozoic) is associated by the openings of back-arc and marginal basins in the overriding
plate (Laurasia-Eurasia) during the Mesozoic (Black Sea, Great Caucasus, South Caspian, Central
Iran, Amu-Darya and Tadjik basins).
The third period is the time of the Cenozoic Alpine collisions involving major continental plates
(Africa, Arabia, India) and Eurasia (Fig.3). The first deformations initiated in the latest Cretaceous-
Paleocene in the Dinarides-Hellenides where minor continental blocks collided with the southern
Moesian attached to Eurasia. The major alpine events initiated in the Early Eocene with the
collision of the (1) northern Indian promontory, and (2) Anatolian blocks with the southern
Eurasian margin, followed by the Arabia-Eurasia collision in the Late Eocene. At the end of the
Eocene, with the ongoing plate convergences, the entire Neo-Tethys oceanic domain was
subducted. Continent-continent collisions were developing all along the southern Eurasian active
margin originating the main alpine chains.
17
THE PERMIAN STRATIGRAPHY OF HAZRO (GONDWANA MARGIN OF
SE TURKEY): FROM FLUVIO-DELTAIC TO CARBONATE RAMP
ENVIRONMENTS, NEW DATA
Baud A., Angiolini L., Broutin J., Crasquin S., Gaillot J., Vachard D.
During the Permian, sequences of terrestrial and marine sediments were deposited within the border
folds domain at the northern edge of the Arabian Platform. Today, a more than 200 m thick
succession is exposed in the Hazro Anticline, close to the front of the Eastern Taurus nappes in SE
Turkey. Based on lithological characteristics these sediments are referred to the Hazro (Kas) and
Gomaniibrik formations and consist of three main sedimentary cycles. The first is built by a lower
fluvio-deltaic complex with thin coal seams. The largely marine transgressive second cycle is
ending with the regressive upper fluvio-deltaic complex. The following third cycle consists of a
marine transgressive, deepening upward carbonate ramp succession, and is topped by a ferruginous
hard-ground developed on an uppermost Permian limestone bed. The Permian part of the Hazro
outcrops is divided into four intervals of time: (a) late Wordian (cycle I); (b) Capitanian (cycle II);
(c) Wuchiapingian and (d) Changhsingian (cycle III). The correlations with the sections studied by
the authors in Zagros (southern Iran) and in Oman allow a more accurate zonation, also based on
sequence stratigraphy.
Concerning the new faunal investigations, detailed Permian algal and foraminiferal studies have
been done by two of the co-authors (Gaillot and Vachard, 2007) and some revisions will be
presented in a pre-congress session (Gaillot et al., this volume). New Middle to Upper Permian
brachiopod data (L. Angiolini, co-author) will be shown in the context of this presentation.
Collaborative palynological researches have been published recently by E. Stolle et al., (2011). A
new macroflora illustration is given by J. Broutin (co-author) that is showing a continuous vegetal
cover with same species during the Middle Permian but apparently without the well-known
Glossopteris in the upper part (upper cycle II, Late Capitanian). Researches on ostracods supervised
by S. Crasquin (co-author) are starting soon.
Our greatly missed colleague J. Marcoux conducted partly the field researches with D. Vaslet and F.
Fluteau. Thanks to our Turkish colleagues M. Bozcu and S. Imamoglu for assistance with the local
administration and help in the field.
18
END-PALEOZOIC EVENTS ON OMAN AND INDIAN GONDWANA
MARGIN
Baud A., Richoz S., Krystyn L.
At the end of the Permian, the carbonate succession of the shallow Oman margin is characterized by
disrupted beds reflecting a response to a specific rheological condition. Half cemented thin beds are
suddenly floating in a fluidized lime mud due to earthquakes shaken. This seismite deposit can be
followed kilometer-on along the Saiq Plateau in the Central Oman Mountains, laterally with
intraformational breccia or distorted structures. Also, along the eastern Oman margin facing the
India-Madagascar rift, outliers of the late Permian deep water Qarari limestone (Batain area) are
surrounded by whitish quartzitic sandstone similar to the white sandstone of the end-Permian
Chhidru Formation of the Salt Range, on the Indian margin side. Close to Asselah, the topmost
Qarari limestone (latest Permian, C. Henderson written communication) is showing conglomeratic
and disrupted beds, laterally extending to a thick debris flow type clast-supported conglomerate
made of exclusively early to late Permian calcareous pebbles in quartz sandy matrix – the Asselah
conglomerate of Hauser et al. (2002).
The seismites described by Brookfield et al. (2013), from the top of the Permian Zewan Formation
at Guryul Ravine on the Indian margin in Kashmir, are apparently of same age. Comparison with
the Oman seismites also suggested that the seismic activity was driven by recurrent phases of syn-
sedimentary block faulting of the northern Indian passive margin.
These earthquakes caused by strong tectonic activity at the Permian-Triassic transition on both the
Arabian margin in Oman and on the Indian margin in Kashmir occurred in close connection to the
main end-Permian extinction level with large climatic and geochemical changes.
19
LATE PALAEOZOIC TERRESTRIAL VERTEBRATE FAUNA: A GLOBAL
VIEW FROM AN ITALIAN PERSPECTIVE
Bernardi M., Petti F.M.
The late Palaeozoic terrestrial tetrapod faunas have been described since long as a discrete
“evolutionary phase” (e.g. Benton, 1985). Ranging from the latest Devonian to the end of the Era
(and beyond), these associations are typically characterized by the dominance of temnospondyl
amphibians, basal reptiliomorpha, non mammalian-therapsids, and anapsids.
Though this view has been challenged by recent findings, we herein provide a comprehensive
overview on the evolutionary trends showed by these taxa during the last 150 Myr of the
Palaeozoic Era, using the perspective of the “Italian” record. During the Carboniferous, amphibians
became diverse and widespread and the first amniotes appeared and diversified. This is highlighted
globally by the skeletal record of popular localities in Europe and Northern America, and is
mirrored in the Italian footprint record described from Sardinia and Friuli (Carnian Alps) which
document the presence of temnospondyls and rare lepospondyls.
Both environmental (driven by wet-and-dry seasonal climate) and geodynamic factors, (linked to
the early rifting phase of the North Atlantic and associated systems), constrained the evolution of
Central Pangaean Pennsylvanian-to-Cisuralian terrestrial faunas that show a cosmopolitan
Euramerican distribution, as suggested also by the recent finding of the huge Alierasaurus ronchii
(Synapsida: Caseidae) in the late Kungurian–Roadian of Sardinia and the footprint-rich deposits of
the well-known tectonically-driven Alpine basins (i.e. Orobic Basin, Collio Basin, Tione Basin,
Tregiovo Basin, Forni-Avoltri Basin and Pramollo Basin).
While the “middle Permian” is poorly documented in this sector of Pangaea, the global aridization
that during the Lopingian drove the substitution of typical hygrophytic Palaeozoic plant groups by
xerophytic Mesozoic groups worldwide, prompted a change in tetrapod faunal composition, from
those dominated by basal synapsids to those dominated by non mammalian-therapsids. While these
latter faunas (and associated diverse terrestrial ecosystems) are best known from the Karoo Basin
(South Africa), and the South Urals (Russia), the Central Pangaean record is documented by the
exceptionally preserved Southern Alpine ichnoassociations, which document the presence of
various groups of non mammalian-therapsids, parareptiles (pareiasaurs) and eureptiles (capthorinids
and neodiapsids) providing one of the best low-latitude record of Late Permian terrestrial faunas.
The finding of archosaur-related ichnotaxa in the Wuchiapingian of the Dolomites region was
recently used to support the hypothesis that archosauriforms, the clade that would have eventually
gave birth to dinosaurs and therefore birds, had already undergone substantial taxonomic
diversification by the Late Permian, providing further evidence for the key role of Central Pangaean
record in the understanding of Late Palaeozoic palaeobiogeography and evolutionary trends, and
highlighting the importance of integrating track and body fossil records in the description of
terrestrial associations worldwide.
20
STRATIGRAPHIC EVIDENCE OF THE LATE PALAEOZOIC ACTIVE
MARGIN IN NE IRAN: CONSTRAINTS ON THE RECONSTRUCTION
OF THE NORTHER SIDE OF THE PALAEOTETHYS
Berra F., Zanchetta S., Zanchi A., Bergomi M., Nicora A., Heidarzadeh G.
The Cimmerian orogen resulted from the collision and accretion of several Perigondwanan blocks
to the southern margin of Eurasia between the Late Triassic and Early Jurassic, following the
closure of the Palaeotethys ocean. Remnants of this orogen discontinuously crop out in N (Alborz
range) and NE Iran (Mashhad–Fariman area) below the syn- to post-collisional clastic successions
of the Shemshak Group (Upper Triassic–Middle Jurassic) and the Kashaf Rud Formation
(Bajocian). In NE Iran rock associations exposed in the Binalood Mountains, Fariman and Darreh
Anjir areas include mafic–ultramafic intrusive rocks, basalts, silicoclastic turbidites and minor
limestones, which have been interpreted in the past as ophiolitic remnants of the Palaeotethys
ocean. Original stratigraphic, structural, geochemical and geochronological data, described in this
paper, suggest a different interpretation. The volcano-sedimentary units of Fariman (consisting of
an association of carbonate platform successions, basaltic flows and siliciclastic deposits, arranged
in a deepening-upward succession) and Darreh Anjir (where basaltic lava flows and radiolarites are
common) complexes where deposited during Permian in a subsiding. Siliciclastic turbidites
(common in the Fariman complex) derived from the erosion of a magmatic arc and its basement,
interfinger with carbonates and basaltic lava flows with both transitional and calc-alkaline affinity.
The coexistence of magmatic rocks with different geochemical signature and the sedimentary
evolution of the basin can be related to a supra-subduction setting, possibly represented by a fault-
controlled intra-arc basin. The Fariman and the Darreh Anjir complexes are thus interpreted as
remnants of a magmatic arc and related basins developed at the southern Eurasia margin, on top of
the north-directed Palaeotethys subduction zone long before the collision of Iran with Eurasia. They
were later involved in the Cimmerian collision during the Triassic. New radiometric ages obtained
on I-type post-collisional granitoids postdating the collision-related deformational structures
suggest that the suture zone closed before mid-Norian times. Deformation propagated later
northward into the Turan domain involving the Triassic successions of the Aghdarband region.
21
A CHRONOSTRATIGRAPHIC FRAMEWORK FOR THE
CARBONIFEROUS KASHAGAN BUILDUP, PRE-CASPIAN BASIN,
KAZAKHSTAN
Brenckle P.L., Collins J.F.
This presentation summarizes the development and application of a local correlation scheme
(Primorsk Correlation Scheme) that provides a chronostratigraphic framework to enable sequence
stratigraphic correlation of Mississippian-Early Pennsylvanian beds across the Kashagan oil
field/carbonate buildup in western Kazakhstan. Results are based on a multi-well core study of
calcareous foraminifers, algae, and incertae sedis, sampled from approximately 2900 m of whole
core and 91 sidewall cores representing an additional 500 m. The scheme incorporates regional
Russian substage nomenclature, modified to reflect differences in the Kashagan biota and
limitations of the core-drilling program. Modifications include the consolidation of some substages
into undifferentiated intervals within the Tournaisian and Bashkirian and replacement of most late
Visean-early Serpukhovian substages with five biozones, named after the successive local
appearances of the foraminifer Endothyranopsis crassa and the algae Fascifolium pantherinum,
Asteroaoujgalia gibshmanae, Calcifolium okense, and Frustulata asiatica. The scheme is suitable
for use in the cyclical, grain-supported, shallow-water platform beds that form the interior of the
Kashagan buildup and may also have application to other open-marine, shallow-water limestones in
the Pricaspian Basin. Microbial beds at Kashagan occur discontinuously in the outer platform, but
dominate the adjacent upper slope facies where they form massive boundstones and boundstone
breccias from the late Visean onward. They contain an encrusting microbiota that is mostly absent
in coeval inner-platform beds.
22
FIRST RECORD OF CRYPTOSPORES IN POST-HIRNANTIAN (LATEST
ORDOVICIAN-EARLY SILURIAN) SEDIMENTS FROM ETHIOPIA
Brocke R., Bussert R., Steemans P.
Recently discovered outcrops of post-glacial Early Palaeozoic mudstones in northern Ethiopia have
yielded a well-preserved assemblage of cryptospores (e.g., Rugosphaera rugosa, Segestrespora
laevigata, Tetrahedraletes medinensis, Velatitetras laevigata and V. retimembrana). These
palynomorphs represent the first biostratigraphic evidence of Early Palaeozoic sediments in NE
Africa and have the potential to shed light on the post-Hirnantian plant colonization of Gondwana.
The mudstones overlay glaciogenic sediments of the end Ordovician (Hirnantian) glaciation in form
of channel fills up to 20 m thick and several hundred meters wide. Laterally the mudstones thin-out
or are completely absent. The basal part of the succession consists of glacially influenced sand-, and
mudstones that are overlain by grey to yellow sand-bearing mudstones of probably Silurian age.
The succession is truncated by cross-bedded sandstones with marine trace fossils, e.g.
Arthrophycus, and locally by a basal layer of quartz pebbles and overlaid by intensely bioturbated
sandstones.
The palynomorph assemblage is dominated by the enigmatic land-derived cryptospores and colonial
algae of possibly freshwater origin. Typical marine elements such as acritarchs and scolecodonts are
extremely rare, chitinozoans are missing so far. In addition, microscopically pyritized objects of
unknown affinity but of probably primary organic origin occur. They obviously reflect metabolic
products during very early mineralization processes in anaerobic habitats or at oxic-anoxic
interfaces.
We interpret the mudstones as the early post-glacial filling of a relic glacial topography, either of
underfilled glacial troughs or sub-glacial channels in a terrestrial or marginal marine environment.
The sharp contact to the overlying shallow marine sandstones formed as a transgressive ravinement
surface and marks the start of fully marine conditions of an inner shelf environment.
The mudstones are the first indication of sediments in NE Africa east of NW Sudan, likely
correlative to Early Palaeozoic post-glacial shales in North Africa and Arabia. Those are locally
enriched in organic matter and form major regional hydrocarbon source rocks. The overlying
Silurian shelf sandstones document the flooding of far interior regions of Gondwana during a post-
glacial transgression coming from the Palaeotethys caused by the melting of the Hirnantian
Gondwana ice sheet.
23
PHYTO- AND PALAEOGEOGRAPHIC IMPLICATIONS OF
MISSISSIPPIAN MIOSPORE ASSEMBLAGES FROM SAUDI ARABIA
Clayton G., Breuer P., Hooker N.
Saudi Aramco Well 667-44 is a cored stratigraphic borehole drilled in northern Saudi Arabia that
penetrated the entire Mississippian (Lower Carboniferous) Berwath Formation, and which is
intended to serve as a palyno- and lithostratigraphic reference section for this interval in the region.
This report is based on a high-resolution palynostratigraphic investigation undertaken as part of a
joint study between Saudi Aramco and the Commission Internationale de la Microflore du
Paléozoique (C.I.M.P.).
Most Mississippian miospore assemblages from Saudi Arabia are diverse and well preserved but
details of relatively few assemblages have been published and correlation with other areas is
tenuous. Previous attempts to date and correlate Saudi assemblages have mainly utilized the zonal
scheme erected in Libya, but with inconclusive results due to the infrequent occurrence of several of
the zonal index species. The Berwath Formation section in Well 667-44 spans the whole of the
Libyan RT Biozone and parts of the MJ and SG biozones but determination of the boundaries of
these zones is difficult for the reasons outlined above. Many miospore taxa previously recorded in
open nomenclature from Saudi Arabian assemblages were formally described in a detailed account
of the Mississippian palynology of the Amazonas Basin, northern Brazil by Playford and Melo
(2012). However, the Brazilian zonal scheme erected by these authors is inapplicable in Saudi
Arabia where a new zonation is being established.
In an important development, Playford (in press) has described a late Viséan–early Serpukhovian
Grandispora maculosa Assemblage that can be recognized in several parts of the Gondwana
Supercontinent, including Brazil, Argentina and Western Australia. However, the existence of this
assemblage along the northern margin of Gondwana between Algeria and Saudi Arabia is uncertain.
The occurrences and relative abundances of characteristic G. maculosa Assemblage taxa in Well
667-44 are documented and reasons for compositional differences compared to the Australian and
South American assemblages are discussed.
24
BIOSTRATIGRAPHIC INVESTIGATION OF THE MILA FORMATION
ALONG THE SHAHMIRZAD SECTION, NORTH OF SEMNAN WITH
SPECIAL REFERENCE TO CONODONTS
Fazli L., Rezaiparto K.
The upper Lower Cambrian to Lower Ordovician Mila Formation is well exposed in the
Shahmirzad section, and it consists of 5 members. Several conodont biozones have been identified
along this section.
Furthermore, several body fossils and tracefossils have been collected from member 2 – 5 of this
section.
Member 1, consisting of stromotolitic dolostone, contains at least one paleosol in the middle part.
The second member which bears several beds of salt pseudomorphs, does not contain any condont,
but trilobites as well as trace fossils such as Rusophycus isp., and Cruziana isp. are frequent). These
trace fossils which are characteristic of the Cruziana ichnofacies suggest shallow marine
environments. Eocrinoids debris as well as epirelief of the roots of these fossils strongly supports
this interpretation. Presence of stormbeds and oriented deposition of Hyolithids, also indicate high
hydrodynamic energy in the sedimentary environment.
Four conodont biozones have been identified from members 3-5. All conodonts obtained from this
section are Paraconodont.
Conodont alteration index in this section is 1-1.5 and suggests temperature of 50 to 90°C s and the
potential of oil.
25
AN OVERVIEW OF DEVONIAN TO PERMIAN IN ALBORZ MOUNTAINS,
NORTH IRAN
Gaetani M.
The Devonian in the Alborz Mountains is represented by a shallow water succession, initially of
clastic and then mostly carbonatic sediments, deposed by a marine transgression on the region
from North-East. The most complete sections are in the East. The base consists of about 130 m of
whitish quartzarenites, overlaid by finer clastics, arenites, siltstone and shale, some 140 m thick.
Few fossils have been detected in the Padeha Formation, mostly in the upper part and suggest an
Eifelian age. Moving up and to the west, the transgression gradually expanded during the Givetian,
reaching the central part of the range during the Frasnian. The Khoshyeilagh Formation is a very
thick (> 1000 m) unit, in which at least three main subdivisions may be identified, two mostly
carbonatic, separated by one arenitic member, mostly of Frasnian age. Other fine terrigenous
intercalations sparsely occur though the succession. Thickness is reduced moving westwards. The
Famennian part is usually thicker and rich in marine shallow water biota. Basaltic outpouring may
occur around the end of the period.
The Khoshyeilagh Fm. ends in the basal Carboniferous, giving way to a pretty carbonatic unit, the
Mobarak Fm. This unit may reach 400-500 in thickness and consists of two parts, more shaley
below and calcareous above, in Central Alborz. These subdivisions are inverted in the eastern
Alborz, where we have the more complete and thick sections: limestone below, marl and shale
above. The documented age are Tournaisian and Visean. The foraminiferal content allowed to
recognize that to the south sections are less extended upwards in their age, only early Visean being
present, or even only the late Tournaisian. Moving north, sections are more complete, extending up
to the late Visean. Later erosion, occurring during the Serpukhovian and/or the late Carboniferous,
has cut the upper part of the Carboniferous section. On the northern side of the range, either for the
vegetation cover, either for the increasing subsequent deformation, the analysis of the succession
interposed between Mobarak Fm. and Dorud Group, is not yet fully done. There are two units,
Dodzehband and Qezelqaleh fms., tens of meter thick, consisting a mixed fine clastic and shallow
water carbonates, that need further research. They occur in the Serpukhovian and Moscovian and
are often bracketed by gaps, also linked to the sea-falls due to the Gondwana glaciations.
By the very top of the Carboniferous, sedimentation resumed on the range. Three major cycles are
present. The lowest, starts in the late Gzhelian and is represented by the Dorud Group. A three-fold
subdivision is recognized, with a lower and upper units arenitic and a thicker intermediate, made by
skeletal carbonates, rich in fusulinids and brachiopods. Asselian to Sakmarian in age. The top of the
Dorud Group is sealed by a lateritic horizon, testifying to a regional emersion under
equatorial/tropical climate. The second cycle is represented by the Ruteh Fm. consisting of a thick
package of wackestone/packstone deposed on a carbonate ramp. Towards the top, locally basaltic
lava flows are present. The top of the cycle is once more made by a lateritic soil, possibly linked to
the end-Guadalupian sea low-stand. The third marine cycle is made by the Nesen Fm., a marly unit
below, overlaid by cherty limestone above, of Lopingian age. The succession testify to a deepening
of the sea floor northwards. To the East, instead the whole Middle and Upper Permian are
represented by lateritic soils and red arenites, indicating a persistent emersion. The P/T boundary is
well represented in the Elikah Fm. with basal microbialites and spectacular domal stromatolites.
From a paleogeographical point of view, the area was transgressed from the East in the Devonian,
26
gradually turning towards the deepest sea in the Carboniferous and Permian existing to the North,
facing the Paleo-Tethys Ocean, before the final docking to the Turan Plate in the Late Triassic. The
northwards rotation of the area, led the Alborz through the equatorial latitudes, where the climatic
control was significant in the alteration of the emergent areas.
27
MIDDLE-LATE PERMIAN BIOSTRATIGRAPHY (ALGAE AND
FORAMINIFERS) OF THE HAZRO SECTION (SOUTHEASTERN
TURKEY)
Gaillot J., Vachard D., Baud A.
The marine fossiliferous Permian part of the Hazro section is divided into three intervals of time: (a)
Capitanian; (b) Wuchiapingan; (c) Changhsingian, based on the assemblages of foraminifers and
algae. The correlations with the sections studied by the authors in Zagros (southern Iran), United
Arabic Emirates and Saudi Arabia allow a more accurate zonation, with introduction of elements of
sequence stratigraphy. The described algal and foraminiferal taxa are:
(1) twenty two new and poorly known genera: Evlaniopsis Vachard in Vachard and Montenat,
1981, Anthracoporellopsis Malov, 1956, Praedonezella Kulik, 1973, Donezella Maslov, 1929
emend. herein, Turkomia n. gen., Foliophycopsis n. gen., Siphoglobivalvulina Gaillot and Vachard,
2007, Septoglobivalvulina Lin, 1978 emend. Gaillot and Vachard, 2007, Retroseptellina Gaillot and
Vachard, 2007, Louisettita Altıner and Brönniman, 1980 emend. Gaillot & Vachard, 2007,
Siphodagmarita Gaillot and Vachard, 2007, Okimuraites Reitlinger in Vdovenko et al., 1993 (=
Brunsispirella Gaillot and Vachard, 2007, Hoyenella Rettori, 1994 emend. Gaillot and Vachard,
2007, Neodiscus Miklukho-Maklay, 1953 emend. Gaillot and Vachard, 2007, Crassispirella Gaillot
and Vachard, 2007, Crassiglomella Gaillot and Vachard, 2007, Uralogordius Gaillot and Vachard,
2007, Neodiscopsis Gaillot and Vachard, 2007, Glomomidiellopsis Gaillot and Vachard, 2007,
Tauridia, Sellier de Civrieux and Dessauvagie, 1965, Polarisella Mamet and Pinard, 1992 emend.
Gaillot and Vachard, 2007, Ichthyofrondina Vachard in Vachard and Ferrière, 1991 emend. Gaillot
and Vachard, 2007, Nestellorella Gaillot and Vachard, 2007, Cryptoseptida Sellier de Civrieux and
Dessauvagie, 1965, and Aulacophloia Gaillot and Vachard, 2007;
(2) fiveteen new species: Foliophycopsis guevencii n. sp., Siphoglobivalvulina baudi Gaillot and
Vachard, 2007, Siphodagmarita vasleti Gaillot and Vachard, 2007, Louisettita extraordinaria
Gaillot and Vachard, 2007, Louisettita ultima Gaillot and Vachard, 2007, Paradagmarita simplex
Gaillot and Vachard, 2007, Paradagmarita planispiralis Gaillot and Vachard, 2007, Hoyenella laxa
Gaillot and Vachard, 2007, Crassispirella hughesi Gaillot and Vachard, 2007, Glomomidiellopsis
uenoi Gaillot and Vachard, 2007, Neodiscopsis canutii Gaillot and Vachard, 2007, Rectostipulina
syzranaeformis Gaillot and Vachard, 2007, Cryptomorphina hazroensis Gaillot and Vachard, 2007,
Pachyphloia enormis Gaillot and Vachard, 2007, and Aulacophloia martiniae Gaillot and Vachard,
2007.
28
PRELIMINARY DISCUSSION ON PERMIAN FORAMINIFERAL
ASSEMBLAGES IN NW AND CENTRAL IRAN
Gennari V., Rettori R., Angiolini L., Ghorbani M.
Several middle to upper Permian stratigraphic successions cropping out in Central and NW Iran
have been investigated in order to define differences and affinities among foraminiferal
assemblages. Our preliminary results point out a difference in the taxonomic diversity of the two
areas. In the Shahreza and Abadeh (Central Iran) successions, we have recorded five orders of
foraminifers, belonging to the class Fusulinata and Miliolata whose diversification is at genus level.
In Shahreza 13 families, 21 genera and in Abadeh 14 families, 36 genera have been recorded in
comparison to Zal (Julfa, NW Iran), where we have found 22 families and 58 genera. In Central
Iran macroforaminifers show a higher diversity whilst the diversification of small foraminifers is
low. The distribution and diversification of small foraminifers allow stratigraphic correlations
among the successions of NW Iran where large foraminifers are scattered or sometimes absent. The
diversity of small foraminifers in these areas which belongs to the same palaeogeographic domain
seem to be due to palaeoecologic and palaeooceanographic conditions. We have also preliminarily
observed that about 25 genera of small foraminifers are typical of NW Iran and no genus is
exclusively present in Central Iran. All the small size foraminifers present in Central Iran are also
present in NW Iran. It could be due that cosmopolitan and endemic genera are respectively “r and k
stategists” and their selection could be related to their nepionic stage. These preliminary results
about a reduced generic diversification in Central Iran in comparison to NW Iran are also confirmed
by brachiopods which show an analogous trend of generic diversification.
29
PALAEOZOIC GRANITOID IN IRANIAN PART OF GONDWANALAND
Ghalamghash J.
Paleozoic granitoids formed during Cambrian and Carboniferous-Permian time in Iran as northern
part of Gondwana. The Cambrian Granitoids crop out in Central Iran zones. These plutons formed
two separate calc-alkaline and alkaline suites. Kuh-e-Polo, Ariz, Kuh-e-Sefid, Kalmard are first
suite that display relatively high LILE/HFSE and LREE/HREE ratios, coupled with negative Ta, Nb
and Ti anomalies in chondrite normalized diagrams. These chemical signatures show a subduction-
zone component and assumed to form in subduction zone in Gondwanaland. Zarigan, Chadormalo
and Narigan alkaline plutons are A- and S-type granite that formed by partial melting of Early
Cambrian crust in central Iran. The Moro, Mishu, Heris and Touyeh-Darvar in Alborz-Azerbaijan
zone and Ghoshchi, Khalifan and Hassanrobat plutons in Sanandaj-Sirjan zones which emplaced in
315 to 288 Ma. They are composite plutons that formed in extensional tectonic setting in Northern
part of Gondwanaland.
30
FUSULINIDS FROM LATE CARBONIFEROUS AND EARLY PERMIAN OF
COLOMBIA
Gómez Cruz A., Moreno-Sánchez M., Lemus-Restrepo A., Vachard D.
Here is presented biostratigraphic information about five localities of the eastern Colombia, three of
Carboniferous age and two of Permian age. The stratigraphic sections and the out crops are
discontinuous, the access is no easy and the sections are tectonically incompletes. It can be
constituted in a starting point to contribute in reconstructing a Late Paleozoic succession of the
north of South America. The studied localities are:
Diamante Formation locality (Rionegro, north of Bucaramanga city). Mud-limestones and black
shales facies with brachiopods, crinoids, bryozoans and foraminifers. Foraminifers includes
Praeskinnerella hedbergi (Thompson & Miller, 1949), Climacammina sp., Schwagerinoidea indet.,
Praeskinnerella transition to Skinnerella sp., Pseudoschwagerina sp., Cuniculinella ex gr.
fusiformis Skinner & Wilde, 1965. This assemblage allows us to assign an Artinskian age to this
locality.
Manaure section (Perija Range, Cesar province). Black shales and limestones facies with fusulinids,
brachiopods, corals and echinoderms. In this section occurs Praeskinnerella hedbergi (Thompson &
Miller, 1949), Pseudoschwagerina dalmussi Thompson & Miller, 1949, Geinitzina? or
Frondicularia sp., Climacammina sp., Tetrataxis sp., Globivalvulina ex gr. bulloides (Brady, 1876);
Globivalvulina ex gr. mosquensis Reitlinger, 1950; Schwagerinoidea indet.; Globivalvulina sp.,
Paraschwagerina sp., Praeskinnerella ? sp. The assemblage is in the Sakmarian-Artinskian age
boundary.
Farallones Group locality (Bogotá-Villavicencio road). Limestones with Fusulinella ex gr.
thompsoni Skinner, 1954, Plectomillerella sp., Schubertellina sp., Fusulinella sp., Pseudostaffella
sp., Climacammina sp., Pseudoacutella cf. grozdilovae (Maslo & Vachard, 1997), Planoendothyra
sp., Palaeotextularia sp., Millerella sp., and Plectomillerella sp. The assemblage belongs to the
Fusulinella zone of Moscovian age (Kashirian and/or Podolskian).
San Antonio Limestones (San Antonio, Huila Province). Mud and oolite limestones and black
shales. The assemblage contains brachiopods, crinoids and Millerellinae foraminifers. Foraminifers
includes Seminovella sp, of early Bashkirian age (Morrowan).
The Paleozoic of La Jagua (Garzón, Huila Province). At this locality the stratigraphic sequences are
interpreted as stratigraphic recurrence of marine and continental environment.
The marine facies are mudstones, sandstones, mud-limestones and oolitic limestones with
brachiopods, trilobites, corals, bryozoans, gastropods, and conularia. There are small foraminifers
of the species Millerella marblensis, Millerella extensa, Planoendothyra aljutovica, Endothyra sp.,
Endothyranella sp., Globivalvulina sp., Eostaffella sp., Asteroarchaediscus ex gr. rugosus,
Calcivertella sp., and Tetrataxis sp.
The continental facies correspond to red mudstones and sandstone with plant remains and
conchostraca (cyzicidae) fossils. The foraminifer assemblage belongs to the Millerella marblensis
zone of Morrowan age (Bashkirian).
These sections represent a marine sedimentation in a wide opened platform in north Gondwana
during the late Paleozoic.
31
CONODONT COLOR ALTERATION MAPS FOR PALAEOZOIC TO EARLY
TRIASSIC DEPOSITS OF THE ALBORZ MTS.
Haghighat N., Hamdi B.
Temperature, based on color alteration index of conodont (CAI), has been determined for the
Alborz sedimentary successions in the following time intervals: Cambrian- Ordovician, Devonian,
Carboniferous, Permian, and Triassic. It was not possible to integrate these C.A.I data into an
isogram. The C.A.I value variation between Paleozoic and Triassic deposits can be explained by
sedimentary burial pressure, tectonic movement, drift above a hot spot, hydrothermal solution, or
even contact metamorphism. Unfortunately, because of scarce data on C.A.I., we were not able to
obtain more achievements in the Alborz Mts. According to this investigation, the presence of
hydrocarbon in the Julfa-Hambast belt is plausible.
32
CLIMATOSTRATIGRAPHY OF THE CARBONIFEROUS–PERMIAN IN
THE EAST GONDWANA INTERIOR RIFT
Haig D.W., Mory A.J.
The East Gondwana interior rift, along which the Indian Ocean formed during the Middle Jurassic
to Early Cretaceous, included major intracratonic Carboniferous and Permian basins that are
preserved on the western margin of the present Australian continent including the Outer Banda Arc,
as well as in various dismembered and now accreted terranes in South-East Asia. The basins of this
rift system provide an archive into the climatic history of the interior of East Gondwana. The
northern basins of the interior rift record a fully marine succession, with known marine facies
becoming more restricted and progressively disappearing toward the south. The best-known
successions are from rift basins, such as the Canning, Southern Carnarvon and Perth basins that
splay from the main axial rift. These were deposited in low-gradient depressions where shallow-
marine to fluvial sedimentation almost kept pace with subsidence. Carboniferous-Permian deposits
toward the main axial rift are covered by a thick Mesozoic-Cenozoic succession and are poorly
known except from Timor where Neogene orogenesis has exposed uppermost Carboniferous and
Permian units within a tectonic melange. Deep seismic on the North West Shelf of Australia as well
as facies present in Timor, suggest that topographically deep rift basins, with several hundred
metres relief, were present in the axial zone of the East Gondwana interior rift.
This talk reviews major climatic trends evidenced by significant changes in marine sedimentary
patterns, floral and faunal distributions and limited stable isotope data. Studied basins lay on a N–S
transect of over 2000 km along which climate signatures are interpreted across a range of marine
palaeoenvironments with variable temporal control. In evaluating the climate record, particular
attention is paid to basin settings and local palaeoenvironmental conditions.
An overall trend from a dry Mississippian to a wet Permian in East Gondwana contrasts with
increasing aridity in central Pangea. The Mississippian was warm whereas the Pennsylvanian
included a substantial period of lowland ice cover (represented by a significant sedimentary hiatus).
The Pennsylvanian glaciation was broadly co-incident with the start of a major episode of rifting
that changed basin architecture from broad sags to narrow rifts and initiated major volcanism in
northern parts of the interior rift. Rapid de-glaciation followed a global warm spike in the Gzhelian
and proceeded in cycles during the Asselian and into the Sakmarian. A temperate wet climate
prevailed during the remainder of the Permian, although there were warm-temperate, sometimes
drier, phases in the late Sakmarian to early Artinskian, late Artinskian to early Kungurian, and in
less well-defined parts of the Wordian–Capitanian, Wuchiapingian and Changhsingian. A cool
interval, with sea ice, was present during the mid Artinskian. The pattern of climate change
recognized in the succession of the East Gondwana rift seems similar to that interpreted from other
parts of East Gondwana.
33
CHARACTERIZATION OF THE MAJOR UNCONFORMITIES OBSERVED
IN PRE-KHUFF PALAEOZOIC SUCCESSION OF THE KUH-E SURMEH
(FARS AREA), KUH-E FARAGHAN AND KUH-E GAHKUM (BANDAR
ABBAS AREA) IN SOUTH OF IRAN
Hasan Goodarzi M.G., Asghari A., Vennin E., Soleimany B., Hajian M.
Palaeozoic series in Fars and Bandar Abbas areas (South of Iran) are well exposed in which are
characterized by distinct sedimentary succession separated by major unconformities and erosional
surfaces. The aim of this study is to interpret these unconformities and erosional surfaces in term of
climate, tectonic events and relative sea level changes and to reconstruct the Iranian
palaeogeography for the Palaeozoic succession.
The first major erosional surface is observed in Kuh-e Gahkum where the Lower most of Early
Silurian fan delta conglomerates and shales corresponding to the Sarchahan Formation, overlies by
a discontinuity pre Silurian (Cambrian in age?) deposits (Motiei, 2003). In the neighbouring Kuh-e
Faraghan, this surface is recorded at the top of the Ordovician Seyahou Formation. This Upper
Ordovician surfaces may be interpreted as a major sea level fall at the end of the Ordovician related
to the Hirnantian glaciation (Ghavidel Syooki et al., 2011). The lateral variations in thicknesses and
facies between the different areas may be related to the local distribution of salt diaper complexes.
The second discontinuity lies at the top of the shallow to deep marine Early Silurian Sarchahan
Formation both in Kuh-e Faraghan and Kuh-e Ghakum. In Kuh-e Surmeh, no Silurian deposits have
been preserved. This discontinuity is related to an uplift of the Middle East area at the end of the
Silurian associated with epeirogenic movements (Al-Sharhan and Nairn, 1997) and an associated
major sea level drop (Haq and Al-Qahtani, 2005).
The third, a major discontinuity separates the continental Early Permian Faraghan Formation from
the older sedimentary Formations (Johnson 2008). In Kuh-e Surmeh, the Early Permian deposit
rests directly on the Ordovician deposits. This area is characterized by the absence of estuarine and
continental and shallow marine clastics Devonian Zakeen Formations. However, drilled wells
located in the surrounding areas (e.g; West Aghar, Naura, Zirreh, Dalan), Devonian Zakeen
Formation as indicated by the palynological studies (Ghavidel Syooki, 1993, 1994, 1998) recorded.
In Kuh-e Gahkum and Kuh-e Faraghan, this hiatus has been confirmed by the absence of the Late
Devonian- Carboniferous deposits (Ghavidel Syooki, 2003) and the Early Permian deposits overlie
the Devonian Zakeen Formation. This surface is generally referred to the “Hercynian
unconformity” (see a recent synthesis by Faqira et al. 2009) spanning from the Late Devonian up to
the Carboniferous (Konert et al. 2001). The absence of almost all the succession between the
Ordovician to the Early Permian in Kuh-e Surmeh, may be interpreted as a consequence of local
salt diapir activity and structuration of salt-related structural high position.
34
MIOSPORE ASSEMBLAGES FROM PŘÍDOLÍAN TO EARLY EIFELIAN
SEQUENCES OF THE OUED SAOURA ALGERIAN SAHARA
Hassan Kermandji A.M., Khelifi Touhami F.
Miospore assemblages from 36 productive samples from exposed sections of Oued Saoura in the
Western Algerian Sahara have been investigated and correlated with previously described palyno-
stratigraphic miospore assemblage biozones of the Tidikelt Plateau, Central Algerian Sahara. Ages
of the studied sequence based on characteristic miospore taxa confirm previously established
limited faunal ages and range from Přídolían to Early Eifelian. The miospore assemblages and the
level of structural complexity of the taxa recorded allow inter-regional correlations to be established
with the uppermost Silurian to Early Eifelian sections from the Illizi, Ghadames and Hammadah
Basins of Algeria, Tunisia and Libya and with other Gondwanan regions with comparable miospore
associations. Assemblage Zone Emphanisporites annulatus-Camarozonotriletes sextatii Richardson
and McGregor retains, in place Emphanisporites annulatus-Geminospora svalbardiae Hassan
Kermandji et al. (preoccupied). Correlations with the Northern Hemisphere are more difficult to
determine. Lacks of productive samples cause precise determination of the Silurian and Devonian
boundary and the position of the Devonian stages difficult to establish.
35
NEW DATA ON THE PALYNOLOGY OF THE DEVONIAN AND
CARBONIFEROUS OF NW-AFRICA (ALGERIA, MAROCCO)
Jäger H.
Several palynological studies were performed in the Palaeozoic of central Algeria and southeast
Marocco. The entire Palaeozoic succession was studied, Carboniferous to Silurian/Ordovician, with
special focus on the Devonian and Carboniferous strata. In central Algeria a set of wells was
studied, representing a margin - basin transect, while in southeast Marocco one well was studied
from the basin margin. All samples are subsurface samples, processed by the same workflow
without any post-maceration processing of the organic residues (e.g. cleaning, oxidising), to avoid
any artifical changes, that could effect the correlation of the different well sections. The studies
included palynostratigraphy, palynofacies and organic maturation analysis to get the maximum
information of the palaeoenvironmental and depositional history of the studied basins.
Palynostratigraphic analysis enabled detailed correlations along the basin - margin transect in
Algeria and long distance correlations with southeast Marocco. It shows an almost continuous
deposition from the Silurian to the Lower Carboniferous with some differences between proximal
and distal wells in Algeria. Minor stratigraphical gaps are observed in the Middle Devonian and
partially at the Devonian- Carboniferous boundary. The uppermost Visean is missing in all studied
wells in Algeria, but is present in the studied well from Marocco. In Algeria the Lower
Carboniferous is overlain by Namurian strata in distal wells, whereas in proximal wells it is overlain
by ?Westphalian strata. Based on palynostratigraphical correlations changes in the sedimentation
rate are observed between proximal and distal wells in Algeria. Distal wells show partially lower
sedimentation rates, especially in the sand-rich intervals of the Lower to Middle Devonian and the
uppermost Devonian (Strunian) to basal Visean.
From the Silurian to the Upper Carboniferous the palynofacies is dominated by terrestrial material,
mainly degraded phytoclasts. In most samples miospores are the most common palynomorphs,
followed by acritarchs and rarely chitinozoa. But preservation of terrestrial palynomorphs is less
compared to marine palynomorphs. Palynofacies shows a general change with time: from distal
shelf to basinal deposition in the Silurian to more proximal shelf deposition during the Lower to
Middle Devonian. This is supported by the change from shale- to sand-dominated deposits. In the
Upper Devonian a shift back to more distal shelf to basinal deposition is observed, dominated by
shales. At the Devonian-Carboniferous boundary a shift towards more proximal environments is
observed again, together with sand-rich deposits. Based on the Terrestrial:Marine Index of
palynomorphs several transgressive events are observed in all wells, which can be used as
additional correlation lines: one in the Upper Silurian, one in the Givetian, four to five in the Upper
Devonian, and one in the Lower Carboniferous (Visean). Other palynofacies proxies have shown
less potential as additional correlation tools.
Organic matter is generally relatively high mature, as indicated by medium- to dark- brown
palynomorph colours and vitrinite reflectance. Organic maturation shows slightly increasing
palaeotemperatures downward, indicating long-term burial maturation controlled by basin
subsidence. Some clearly confined intervals show intense secondary thermal overprint, most
probably due to magmatic intrusions of the Mesozoic CAMP volcanism.
36
OPTICAL KEROGEN ANALYSIS FOR ENHANCED ANALYSIS OF
HYDROCARBON SYSTEMS: FROM MATURE EUROPEAN BASINS TO
NEW EXPLORATION IN NORTHERN GONDWANA
Jäger H.
Palaeozoic basins throughout Europe are targets of intense research for quite a long time, regarding
stratigraphy, sedimentology, structural geology and basin evolution, but also exploration of
different resources like coal, minerals, metals and hydrocarbons. Hydrocarbon exploration started as
early as in the early 20th century including intensive geophysical subsurface analysis (well logs,
seismic lines) and geochemical analysis of potential source and reservoir rocks, leading to highly
mature explored basins. Nevertheless in recent years new exploration activities for unconventional
hydrocarbon shale plays in Europe showed a very strong mismatch between the expectations based
on the established data and basin models and the results of recent exploration activities. This shows
a strong need for new, enhanced exploration workflows to better understand the problems of the
classically used models and methods and to improve the level of reliability and risk minimizing in
future exploration.
A very promising workflow for enhanced hydrocarbon system analysis is Optical Kerogen
Analysis, based on optical analysis of kerogen composition, preservation and maturation. Kerogen
composition provides the detailed quantification of each kerogen type within the total kerogen of
each sample, the quantification of productive vs. unproductive proportions of the total kerogen
(=net TOC) and the quantification of oil-prone vs. gas-prone kerogen. Analysis of kerogen
preservation indicates the level of hydrocarbon transformation and for unconventional shale plays,
it also indicates the storage capacity, depending mainly on kerogen microporosity. Detailed
maturation analysis is based on integrated organic maturation analysis, double-checked by two
independent methods for maximum reliability and application. Optical kerogen analysis identifies
different kerogens with different hydrocarbon potential mixed within the total kerogen of each
sample, enhancing significantly the resolution and reliability of kerogen analysis and the evaluation
of the hydrocarbon potential compared to bulk-rock geochemical analysis.
Two case studies are presented from Palaeozoic basins of central Europe: the Carboniferous of the
North German Basin and the early Palaeozoic (Ordovician-Silurian) of Poland. Both are highly
explored basins with huge data sets produced by classical workflows used in past exploration.
Nevertheless recent exploration showed major misfits between expectations and exploration results,
struggling mainly due to problems with kerogen quality (composition) and basin maturation.
Optical Kerogen Analysis was performed focused on these two topics to enhance the reliability of
the hydrocarbon potential analysis and to avoid the pitfalls caused by standard geochemical
exploration workflows. The results led to major changes in both basins, regarding kerogen
composition / quality (type of the produceable hydrocarbons) and basin maturation. Maturation
changed from upper gas / overmature to upper oil window in the North German Basin and lower /
middle gas to lower / middle oil window in Poland. Together with the results of kerogen
composition this led to a locally prolific oil-shale play in the early Palaeozoic of Poland and to an
unproductive unconventional shale system in the North German. Therefore detailed optical kerogen
analysis shows very high potential to improve hydrocarbon system analysis and reduce exploration
risk of hydrocarbon plays significantly.
37
LATE PRECAMBRIAN-EARLY PALEOZOIC STRATIGRAPHY OF
NORTHERN GONDWANA REGION WITH SPECIAL EMPHASIS ON
IRAN
Kani A., Ghorbani M.
The oldest known rocks with definite stratigraphic affinity in Northern Gondwana, in general, and
Iran, in particular, are those of Neoproterozoic which are represented by various igneous,
metamorphic and sedimentary units.
In Iran, during the final stages of Pan-African Orogeny, whose record can be seen in most of North
Gondwanan terranes, an intracontinental rift was developed in an extensional setting during the
deposition of Kahar Fm. (Alborz), Tashk Fm. and Kalmard Fm. (Central Iran) and their equivalents
in other parts of Northern Gondwana. The results of this rift were formation of volcanic rocks of
Qaredash, Rizu, Desu and Hormuz series and their intrusive equivalents. Simultaneous with the
closure of this rift, platformal conditions prevailed over most of these terranes that lasted till end of
Early Paleozoic. The shallow platformal successions that were formed within this rift system
include Soltanieh Fm., Barut Fm., Zaigun Fm. Lalun Fm. and Mila Fm. along with their equivalent
facies (with minor differences) exposed all over Iran and its neighbouring countries. Following the
closure of this rift which was similar to present-day Red Sea, the oceanic crustal rocks and the
overlying sediments were deformed and metamorphosed resulting in the successions of Anarak and
Takab regions (where the oceanic crust was exposed within the rift. Other platformal sediments
were also metamorphosed, but to a lesser extent (the effects are seen in Kahar Fm. of Alborz and
Kalmard Fm. and Tashk Fm. of Central Iran).
Closure of this rift results in development of platform environments all over Iran, and probably the
Northern Gondwana, leading to deposition of shallow marine (or continental) sediments. Such basin
reaches their maximum extension in Cambrian times with deposition of Lalun sandstones and its
equivalents which extend almost all over the Middle East.
These developments can be attributed to Pan-African Orogenic cycle in Northern Gondwana.
38
A SUMMARY OF THE CURRENT INVESTIGATIONS ON PALAEOZOIC
ROCKS OF IRAN
Kani A., Ghorbani M.
With establishment of National Iranian Oil Company (NIOC) in 1948 and Geological Survey of
Iran (GSI) in 1959, the new era of geological investigations began in Iran. The NIOC focused on
the Cenozoic and Mesozoic sedimentary successions with the aim of discovering new hydrocarbon
reserves, while GSI’s objectives were more general encompassing all the geological aspects of the
country. With advancement of academic institutions, a large volume of geological work has also
been carried out by the universities in form of M.S. and Ph.D. dissertations.
In spite of all these efforts, paleontological and stratigraphic studies always represented an
inconsequential part of regional geological investigations. The only exception being the work of
Wynd on the biostratigraphy of Mesozoic and Cenozoic rocks of Zagros Basin carried out in the
early 1960s.
The Project titled “Palaeontology and Stratigraphy of Paleaozoic Successions of Central Iran and
Zagros Basin” commenced in the year 2012 by Arianzamin is aimed at systematic studies to
through light on hydrocarbon potentials of these rocks. Since then, fifty-Six surface sections of
Paleozoic succession have been sampled for their micro- and macrofossil contents, and over 15000
samples have been collected and studies. Moreover, the samples of 13 sub-surface boreholes, drilled
by NIOC in previous years, that contained Paleozoic sequences have also been re-examined. The
project has currently reached its final stages and the obtained data are being compiled in order to
achieve regional correlation and delineate paleogeographic framework for the Paleozoic rocks of
Iran. Moreover, the collected samples will be subjected to sedimentological and geochemical
investigations in the next phase of the project to reveal their hydrocarbon potentials.
39
THE CONTINUITY OF RIFTING PHASE AND ITS IMPACT ON
HYDROCARBON DISTRIBUTION DURING THE CARPITANIAN IN
THE FARS PLATFORM OF THE ZAGROS FOLD BELT, SW IRAN
Kavoosi M.A.
The Upper Permian Dalan Formation is an economically significant gas and condensate reservoir,
which deposited on the passive margin of the Neo-Tethys Ocean, NE Gondwana. During Late
Permian period, the Gondwanaland broke up and the Paleo-Tethys started opening, which led
establishment a carbonate platform and deposition of the Dalan Formation along the northeast
Arabian Platform. The sediments accumulated within the Carpitanian time interval, comprise the
Nar Member of the Dalan Formation that is distributed in the Zagros fold belt and Persian Gulf,
southwest Iran. The Carpitanian Nar Member approximate equivalent of Khuff anhydrite ranges its
thickness between 80 to 320 metres. The Nar Member has recorded important evidence of the
geodynamic and palaeogeography to understand the hydrocarbon reservoir distribution in the
Zagros fold-thrust belt. From petroleum point of view, the basin evolution, carbonate platform and
depositional environments play a main role on hydrocarbon systems.
The member comprises carbonates, gypsum/anhydrite and subordinate sandstone. Detailed field
surveys, microscopic studies, wireline logs and facies analyses were used to investigate the
depositional environments and impact of rift phase on the reservoir distribution. Facies analysis of
the member led to the recognition of microfacies related to the coastal plain, tidal flat, lagoon, and
shoal facies belts deposited on a ramp carbonate platform. In the outcrop (Surmeh Mountain), the
sandstone within the Nar Member represents basal erosive surface, low-angle, planar-laminated
indicating the flood-tidal beach depositional environment. Petrographical investigations reveal
sandstones composed mainly of basaltic rock fragments, unaltered and altered plagioclase, embayed
quartz crystals, volcanic glasses and ashes. The continuity of rift phase is in line with considerable
distribution of the mafic volcanic rock fragments, tuffs, and sandstone in the Nar Member of the
Zagros fold-thrust belt. This evidence can be attributed to the beginning of tectonic instability
consistent with volcanic activity and continuation of rifting/rifting pulse during Late Permian. The
continuation of rifting led to block-faulting and creation of local highs and lows with different
thickness and lithofacies/microfacies variation. The establishment of shallow and restricted
conditions together with arid conditions resulted in formation of evaporites. The radiolarian
wackestone/packstone facies in the lagoonal environment and evaporite deposits brings the idea that
continental rifting supplied considerable SiO2 and sulphur in the sea-water for evaporite deposition
and radiolarian bloom under restricted conditions.
According to obtained data from drilled exploration wells, there is a relationship between the Nar
Member palaeogeography and distribution of the reservoir zones and kind of hydrocarbon in the
overlying Dalan carbonates. In the Fars platform, most of gas reservoirs are located on palaeohighs,
meanwhile; oil and condensate reservoirs and dry wells locate peripheral of the palaeohighs and
flanks, respectively. The high pressure of gas in the palaeohighs led to downward movement of oil
into the anticlines located in peripheral of the palaeohighs, which had lower palaeogeography
during deposition of the Nar Member and upper Dalan carbonates.
40
EXTENSIONAL MOVEMENTS DURING THE EARLY MIDDLE
CAMBRIAN RECORDED IN THE MEMBER 1 OF MILA FORMATION
IN THE EASTERN ALBORZ MOUNTAIN RANGE
Kavoosi M.A., Shamani F.
This study carried out in the northeast of Damghan city at the Baba Ali outcrop section in the
southern limb of Eastern Alborz Mountain Range of north Iran. The study area was situated on the
north of the Gondwana supercontinent. The Member 1 of the Mila Formation (late Lower
Cambrian) with a total thickness of 127 metres consists mainly of thin- to massive-bedded brown
dolostone, dolomitic limestone, and limestone with yellow marl interbeds. The lower contact with
the top quartzite sandstones is gradational. Meanwhile, its upper contact with the Member 2
represents a discontinuity surface together with sharp lithological changes from carbonates to marl.
Detailed field surveys and petrographic investigations led to recognition of several microfacies
related to tidal flat, lagoonal and shoal facies belts. The facies were deposited on a carbonate ramp
under arid conditions similar to the present day of Persian Gulf.
The global sea-level rise in the early Middle Cambrian resulted in carbonate platform establishment
and deposition of the Member 1. The overall thickening-upward of succession is attributed to
continuous sea-level rise. We recognized two regressive events in the Member 1 of the Mila
Formation. The lower cycle comprises very shallow marine carbonate including the stromatolite
and microbiolite boundstone, hybrid sandstone, peloid intraclast grainstone/packstone, and solution
breccias. The upper cycle comprises lime mudstone with evaporite pseudomorphs, oncoid
packstone, microbiolite boundstone/bioherm, peloid packstone, intraclast packstone, and bioclastic
grainstone.
Field surveys and petrographic investigations represent syn-depositional normal faults of
microscopic- and macroscopic-scale in the carbonate of the upper cycle. The syn-depositional
normal displacements are attributed to extensional movements during deposition of the Member 1.
It is nevertheless interesting to note that lateral thickness changes and even non-deposition of the
Mila Formation in other parts of the Alborz most likely suggest block faulting related to extensional
movements along the passive margin of the Proto-paleoetethys margin.
41
LATE DEVONIAN ORGANIC-WALLED MICROPLANKTON FROM
CENTRAL PORTUGAL AND ITS IMPLICATIONS ON
PALEOGEOGRAPHY
Machado G., Vavrdova M.
The organic-walled microplankton described in this work derives from the slates of the Albergaria-
a-Velha low-grade metamorphic Unit (AVU) that crops out in Central Western Portugal. The
palynological content is invariably heavily matured, and spores are generally black and opaque,
although some thin walled ones retain some translucency. The organic residue was composed, in
most instances, by semi-translucent dark grey to black AOM with subordinate amounts of
sporomorphs and acritarchs (s.l.), which were very often fragmented and unsuitable for taxonomic
determination. Phytoclasts are generally rare. Acritarchs and prasinophytes are present in most
samples with ages from the Frasnian to the Early Tournaisian and are exceptionally diverse and
abundant in some samples. The preservation is poor to moderate in most samples, although a few
samples showed moderate to good preservation. These were preferably used for the taxonomic
work.
The assemblage from multiple samples of the AVU contains over 50 different acritarch and
prasinophyte species. Prasinophyte phycomata are invariably small or very small (5 to 15μm),
except for some Dictyotidium spp., which may be up to 40μm.
Previous qualitative analysis of the assemblage points to an affinity with the Laurussian late
Devonian marine Realm, in contrast with the Late Devonian assemblages from the South
Portuguese Zone (less than 300km away today), which shows affinities with North Gondwana.
In this work we compare the AVU assemblage – in a quantitative way - with other Late Devonian
assemblages from sedimentary basins in Iberia (Portugal and Spain), Northern Europe (Belgium,
France, Germany), North America (USA and Canada), Brazil, Colombia, North Africa (Algeria and
Lybia), Iran, Australia and China. Cluster analysis was performed using PAST (Palaeontological
Statistics Freeware).
The results show low similarity values of the clusters, reflecting the cosmopolitan nature of Late
Devonian organic-walled microfossils. Despite these results, several clusters are evident pointing to
a closer affinity of the AVU assemblage with Eastern USA basins’ assemblages and Northern
Europe assemblages. Specifically the affinity of the AVU assemblage is indicated by the presence
of Cymatiosphaera perimembrana Staplin, 1961; Uncinisphaera (Villosacapsula) ceratioides
(Stockmans & Willière) Colbath, 1990; Winwaloeusia cf. ranulaeforma Martin, 1984 and other
acritarch genera and species described from Central and Northern Europe (especially Belgium –
Ardennes-Rhenish massif) and Eastern USA and a complete absence of species of Horologinella
and Schizocystia (common Gondwanan genera).
42
SEQUENCE STRATIGRAPHY OF THE PERMIAN-TRIASSIC BOUNDARY
IN THE CENTRAL PERSIAN GULF: NEW INSIGHTS FROM A NOVEL
AND INTEGRATED APPROACHES
Mazaheri Johari M., Moradi M., Bahrammanesh Tehrani M., Eidani M.
The Permian–Triassic boundary is a world-wide extinction event in the history of life while this
renowned boundary is recorded as a geology feature in the Central Persian Gulf which plays a key
role in the reservoirs characterization. In this research an integrated approach including
stratigraphy-sedimentary studies (micropaleontology, petrography and sedimentary environment)
and a semi-intelligent method based on improving of conventional well logs has been applied in
order to sequence stratigraphy, relative changes in sea level and large-scale changes in the Central
Persian Gulf sedimentary environments. On the one hand, lack of comprehensive data and the high
cost of high resolution data (Formation Micro Imagers and cores), and beside high dependence on
knowledge of interpreters lead to employment of the semi-intelligent method to develop geological
interpretations on limited number of wells to the more wells and the hydrocarbon fields.
At the first place, the semi-intelligent method has been developed to a quantitative stratigraphy by
mathematical improving of row gamma ray logs. Eventually, it led to creation of a novel log, which
illustrates relative change of sea level. Secondly, we have achieved a clear interpretation by
integrating the result and conventional geological evaluation, relatively.
Comprehensive investigations on the thin sections in some wells revealed 11 microfacies related to
five Facies belts from Sabkha to Open marine areas, and also five biozones including Shanita amosi
Range zone, Paraglobivalvulina mira Range zone, Paradagmarita monodi Range Zone and
Charliella altineri Interval Zone for Upper Dalan Formation and Spirorbis phlyctaenae Range Zone
for Kangan Formation for these Permo-Triassic sequences. On the base of the differentiated
biozones an age of Late Midian – Late Djulfian for the Dalan and Anisian for the Kangan
Formation is confirmed. Dorashamian and Scytian strata were not determined in this study
confirming a gap between the two formations belongs to abrupt sea level change in Permo-Triassic
boundary.
However, integration of the interpretations (facies, sedimentary environment, micropaleontology
and semi-intelligent method) suggested that P-T sediments of the basin include approximately four
third order sequences, but it seems that each well has shown various forth order sequences. The
results have been suggested that the P-T boundary shows-off two different roles in the basin. In
some wells open marine facies has been continued by lagoon and shoal facies. So, gradual decrease
in sea level was determined. In contrast, in some other wells the boundary consists of shoal facies
and anhydrite layers. Therefore, it is likely that the boundary is continued in high-order sequence
(Highstand system tract). Anhydrite layers(is reported previously) located slightly above the
boundary as the issue proved that the third sequence boundary should be shifted to lower part of
Kangan Formation. Apparently, there is a fourth-order sequence where the boundary showed-off as
an erosional surface. Probably, the issue is due to local exposure of the shoals. As an outcome, P-T
sequences showed-off as different role in term of sedimentary environment in south and north of the
Central Persian Gulf.
43
APPLICATION OF THE SOFTWARE TSC TO DEPICT GLOBAL SEA-
LEVEL CHANGES AND SEQUENCES
Moezzi Nasab R., Mohamadi M.
During the life Earth of the sea level has been changed. Changes in sea level has been attributed to
several factors. Geologists using sequence stratigraphy of ocean levels rise and fall time of the
estimate. In this article introduce software that TSC is a wide range of applications, global sea-level
changes and sequences during the Paleozoic, Mesozoic and Cenozoic drawing is displayed.
Software calendar geological stratigraphy and paleontology science researchers suggested.
44
EARLY PALEOZOIC THICKNESS VARIATION CONTROL ON
DEFORMATION STYLE IN THE CENTRAL FARS: IMPLICATIONS
FOR HYDROCARBON RXPLORATION
Motamedi H.
Iran's proved natural gas reserves are about 15.8% of world's total reserves. Significant amount of
non-associated gas reserves are proven from the well known Permo-Triassic Dehram Group (Khuff
equivalent in Arabia) play across the Fars region, east of the N-S trending deep seated Kazerun
Fault. This play is part of the Paleozoic petroleum system which is sourced by the Silurian hot
shales and sealed by the Triassic Dashtak evaporites. The Gavbandi High (northward continuation
of the Qatar Arc) is associated with the most of onshore giant gas reservoirs in Permo-Triassic
succession.
The deformation pattern of the folded structures in the Central Fars area change dramatically across
the N-S trending Gavbandi High. A complete data set including seismic profiles, well data,
magnetic surveys and field observations were used to address the reason behind this variation. The
results of the magnetic survey in the central Fars shows significant steps in crystalline basement
which controlled the depositional thickness of Cambrian Hormuz salt as well as the Early Paleozoic
succession. The thin Hormuz salt over the Gavbandi High also could explain the lack of the
breached or buried salt domes in this area. Based on the seismic profiles, the total thickness of the
Lower Paleozoic succession in the eastern side of the Gavbandi High is approximately 40-50%
thicker than on the summit of this basement high. The structural style variations in the central Fars
area is found to be related to thickness changes of the Early Paleozoic sedimentary pile as well as
Neo-Proterozoic- Early Cambrian Hormuz series.
In the eastern shoulder of the Gavbandi paleo-high the considerable thickness of the Hormuz salt
increased its efficiency as the basal decollement and decoupled a thick sedimentary pile from the
crystalline basement during the Neogene Zagros orogeny. Progressive shortening during the fold
development was accommodated by evacuation of the salt from the synclinal areas into the core of
the adjacent large wavelength anticlines. As a result all of the other possible decollement layers in
the sedimentary sequence remained inactive and the whole of the sedimentary succession deformed
as a buckled fold with minor thrusting either in the back limb or forelimb of the folds.
In contrast, over the Gavbandi High, where the Hormuz basal decollement layer was very thin or
absent and relatively thin sedimentary cover, welding of the sedimentary pile and the basement in
the synclinal areas occurred much earlier during the fold evolution. As a result, the shallow
decollement levels in the sedimentary cover became activated during the progressive shortening
which resulted in development of multi-decollement folding marked by short wavelength anticlines
with greater complexity of the fold geometry.
The location of prospects in comparison to Pre-Zagros regional and local paleohighs, variation of
structural style in folded traps due to lateral changes in stratigraphy and the time relationship of
hydrocarbon generation and migration to the folded structures during the Zagros orogeny are these
main critical parameters for future exploration in Permo-Triassic play in the Fars area.
45
SHANITA ZONE WITHIN THE MIDDLE-UPPER PERMIAN
CHRONOSTRATIGRAPHIC FRAME IN TURKEY
Özkan-Altiner S., Altıner D., Şahin N.
Shanita, characterized by porcellaneous tests with a streptospirally coiled initial stage followed by a
planispiral and completely involute coiling in the adult and numerous vertical pillars usually
arranged in alternating rows, occurs in a short stratigraphic interval within the Middle-Upper
Permian successions of the Anatolide-Tauride block. Two morphologically distinct species of
Shanita, S. amosi and S. broennimanni, occur in the lime mudstones, bioturbated lime mudstones
and algal and foraminifera wackestones and packstones and are usually associated with forms like
Necdetina taurica, Charliella rossae, Globivalvulina vonderschmitti, Rectoseptellina decrouezae,
Septoglobivalvulina distensa, Dagmarita chanakchiensis, ‘Neohemigordius’ maopingensis,
Midiella broennimanni, Glomomidiella nestellorum, Aulocopholia martiniae, Frondina permica,
Calvezina ottomana, Polarisella elabugae, Rectostipulina pentamerata and several other forms
belonging to Fusulinata, Miliolata and Nadosariata. In one of the studied localities of the eastern
Taurides, Shanita stratigraphically occurs well above the extinction horizon of schwagerinid-type
fusulinoideans (Chusenella, Parafusulina, Skinnerella etc.) corresponding to the mid-Capitanian
and just below the Upper Permian Wuchiapingian stage marked by successively occurring
Paraglobivalvulina mira-Reichelina and Louisettita elegantissima Zones. The Shanita Zone seems
to be an excellent marker of the uppermost Capitanian of the Southern Biofacies Belt in Turkey and
is confined to the Cimmerian Continent and a limited region in the northern Gondwana in the
Permian reconstructions of the Tethys.
46
GEOCHEMISTRY OF IRONOXIDE, APATITE AND REE ELEMENTS
FROM LACKE-SIAH, BAFGH (CENTRAL IRAN)
Pur Nourbakhsh F., Lotfi M., Rezaie Rad A.
The Lacke-Siah magnetite-apatite deposit is situated 40 km NE Bafq. The Lacke-Siah is located in
Bafq-Poshtebadam subzone of Central Iran structural zone. Iron-apatite ore in Siah Caldera
Complex, following the magmatic evolution that has been formed. The complex consists of acidic
pyroclastic rocks, rhyolite-granite domes, quartz porphyry, Magnetite, diabasic, carbonatite
sometimes contain REE, gabbro massive, phosphate dykes and skarn is associated. Magmatic event
of Siah Caldera Complex, on rocks body of Nadygan thermal effect and in some cases, such as
Lacke-Siah metasomatic skarn has been caused.
According to studies, texture, construction and mineral paragenesis of just Dyke, Plug Neck, lava
and pyroclastic is exposed and the magnetite–apatite ore banded textures, veins and veinlets,
disseminated, exsolution, vesicular, replacement, porphyry and mass is visible. The dominant
minerals include magnetite, apatite, actinolite, Ti-oxide, hematite, pyrite, chalcopyrite, bornite and
iron oxide and hydroxide and copper hydrocarbons.the alteration is more obvious in the volcanic
rocks and includes chloritization, argillic alteration, silicification and also formation of mafic
minerals epidote. The host rocks are strongly altered. The host rocks in Lake-Siah area plot on
alkaline-sub alkaline field. Check the spider diagrams and measurement performed on the samples
of rare earth elements is shown upper rate LREE/HREE that it’s magmatic apatite features. REE
pattern of apatite, magnetite and country rocks are similar and magmatic relationship between them
indicate. Fluid inclusion studies were used in the mineral apatite which studies the formation of
magmatic fluids rich deposits of P, Fe and REE have an important role.
Compare the most important characteristics of the Lacke-Siah iron-apatite ore deposit (including the
tectonic setting, host rock, mineralogy, alteration and structure, texture and geochemistry) with the
characteristics of different types of iron mineralization in the world, has shown that deposit apatite-
bearing iron oxide Lacke-Siah, more similar to iron oxide and apatite mineralization type is Kiruna.
47
A TRANSITION FROM PRE-RIFT AND POST-RIFT SEQUENCES IN THE
ZAGROS REGION AND CENTRAL IRAN
Piryaei A.
The Permo-Triassic sedimentary succession of the NE part of Gondwanaland has experienced a
phase of rifting event during which Iranian plates was separated from the Africo-Arabian plate
including Zagros region. A comparison between the Permian Dalan Formation in the Zagros
Foreland Fold Thrust Belt and the Jamal Formation in the Central Iran shows facies similarities in
which thick shallow-water carbonate developed throughout these areas. In the Zagros region, the
Middle to Late Permian Dalalan Formation consists predominantly of reefal to highly fossiliferous
and oolitic and evaporitic facies that occasionally is associated with clastic and dolomitic facies.
The sedimentary facies of the time equivalent Jamal Formation starts with clastic carbonates,
passing through the reefal limestones and ends with dolomitic facies. Both formations are contained
by fusulinid fossils. The presence of sandy and tuffaceous-basic volcanic rocks immediately north-
east of the actual Zagros suture zone could be interpreted as the first sign of rifting event during the
Permian. Following this, in the Early Triassic time the lithological differences between the Central
Iran and Zagros become more appear. A SW-NE trending cross section indicate that at this time the
Kangan Formation with the tidal and shallow water evaporitic and carbonate facies grade to marine
and somehow bituminous shales towards the Zagros Crush Zone. These sedimentary facies are
deposited in an elongated depressed basin almost parallel to the Zagros trend. During the middle
and late Triassic, this basin was widened and host basal Aghar Shale and basinal evaporites of the
overlying Dashtak Formation. These regional evaporites replaced or surrounded laterally by shallow
water carbonates of the time equivalent Khaneh Kat Formation to the basin margin and form one of
the major cap rocks for the underlying Dalan-Kangan (Dehram Group/Khuf) reservoirs. At the
beginning of the Triassic interval of the Central Iran is regionally covered by Sorkh Shale
Formation with carbonate, evaporitic and siliciclastic facies deposited in marginal (lagoonal, tidal
flat) to Playa environments. These facies are overlain by platform carbonate of the Middle to Late
Triassic Shotori Formation with mainly dolomitic facies. In addition to the lithological contrasts
some other evidences such as obducted huge exotic slabs and radiolarite-ophiolitic complex
emphasized that the rifting event is interpreted to be started during the Late Permian up to Early
Triassic. This can be documented by exotic blocks as old as Late Permian in the obducted
sediments (for example in the SW flank of the Kuh-e Dalneshin Anticline in the Interior Fars). The
age and mechanism of rifting is still a controversial issue between the authors. Age analysis of the
radiolarian fauna and associated fossiliferous calciturbidites represent an age range from late
Paleozoic up to Turonian indicating a time interval during which rifting has been taken place. Based
on the aforementioned stratigraphic succession and dating results the incipient trough seems to be
created during the Late Permian to Early Triassic time and continued by Neo-Tethys Ocean
development in later times. Lateral thickness variation along the SW-NE transect passing through
the Fars Area in the central part of the Zagros is also confirmed with existence of a narrow trough
parallel to the Zagros trend.
48
CHARACTERIZATION AND SOURCE ROCK POTENTIAL OF
PALAEOZOIC SEQUENCE IN THE ZAGROS BASIN, IRAN
Rashidi M., Solimany B., Tahmasebi Sarvestani A., Daryabandeh M., Hajian M.
The Zagros fold belt is situated along the NE margin of the Saudi Arabian Plate and is a currently
active compressional belt. The Zagros Fold Belt consists of a folded Paleozoic to Miocene
sedimentary sequence of several thousands of meters thickness, and overlies Infra Cambrian and
early Paleozoic platform sediments upon a Precambrian basement. The Paleozoic sequence contains
very significant source rocks, overall Zagros in Iran owing to the high total organic carbon (TOC)
content of the Seyahoo and Srachahan formations in Bandar Abbas area (Bordenave 2002, 2010,
Jassim and Al-Gailani, 2006). Geochemistry of Paleozoic sequences in high Zagros are unknown.
Only a few unpublished studies exist on the geochemistry of these source rocks so other
information are required for understanding the existence of hydrocarbon resources. In an attempt to
evaluate source rock potential, maturity, kerogen chemical structure to determine the composition
of petroleum hydrocarbons generated from the kerogen and reconstruct the paleoenvironments of
deposition were subjected to detailed geochemical analyses. The Paleozoic sediments include the
Cambrian Mila, the Ordovician Ilebek, Silurian Zard Kuh formations, in high Zagros and
Ordovician Seyahou and Silurian Sarchahan formations in Bandar Abbas, and the Permian
Faraghan and Dalan Formations in both areas.
The TOC values measured on the kerogen residues were 0.1% and 10%, respectively. These values
indicate that the organic matter in these samples consists largely of kerogen.The remaining potential
of Mila, Ilbeck and Zardkuh formations is fair according to TOC values (0.1-1.1 ), but these
samples could have better initial source rock properties assuming their high level of maturity. Most
of the samples from the Bandar-e-Abbas and Kuh-e Surmeh areas have very high Tmax values; thus
these Paleozoic rocks are highly matured and buried in deeper parts of the basin. In contrast,
samples from the High Zagros area have relatively low Tmax values and some of them may be still
placed in the oil window. The Hydrogen Index of samples is very low except for Silurian shale from
Kuh-e Surmeh. The kerogen derived from Mila Cambrian formation and Sarchahan Silurian are
related to marine organisms yield because of mainly aliphatics chains and producing aliphatic
hydrocarbons (condensates and oils). The kerogen of Permian Dalan, Faraghan and Zard-Kuh
samples from Permian to Silurian in high Zagros area derived from terrestrial plant produced alkyl-
phenols in significantly higher amount than the other kerogen. Their original immature kerogen
might be Type III.
Most of the samples show very high expulsion efficiency, with 95 to almost 100% of generated
hydrocarbon expelled. Initial TOC of more than 1% is obtained from the Ordovician and Silurian
shale, especially from the Bandar-e-Abbas area, while the base of the Sarchahan Formation
recorded 10% initial TOC. The vertical distribution of TOC in the Sarchahan Formation is similar
to that in the “Hot Shale”, which is widely observed in rocks that formed the northern Gondwana
margin.
49
HYDROCARBON POTENTIAL AND KEROGEN STRUCTURE
EVALUATION OF PERMIAN FARAGHAN FORMATION IN ZAGROS
BASIN OF IRAN
Rashidi M., Tsuchida K., Daryabandeh M., Ghorbani M.
The Zagros Basin extends around the Persian Gulf upon the Arabian Plate, with its northern limit
marked by the Zagros Main Thrust. The faults divide the Zagros Basin into a number of different
domains. The study area corresponds to the High Zagros, Fars and Bandar Abbas regions, which all
contain outcropping Paleozoic deposits and gas reservoirs. In the study area, Paleozoic sediments
include the Cambrian to Permian Faraghan and Dalan Formations.
The lower Permian Faraghan Formation is widely distributed in the Zagros Basin of Iran. The
thickness of this formation in surface section from north west to south east is 500 m at Chalisheh,
60 m at Zard Kuh, 60 m at Kuh-e Dena in high Zagros. The formation consists mainly of alternating
sandstone and shale and includes coal layers in the Zard Kuh and Chalisheh areas in High Zagros.
For determining of source rock quality and hydrocarbon potential of the Faraghan sedimentary
rocks as probable source rock and defining kerogen structure to evaluate petroleum systems in
Paleozoic sequence, three exposed sections from the High Zagros area and five wells from
Fars,Bandar Abbas and Persian Gulf were selected for Rock Eval and PY-GC analysis. TOC% of
samples in wells, indicates that a great number of samples present range less than 0.5%. The
average HI in all wells is generally less than 115 (mgHC/g rock) in Fars area which indicated Type
III and Gas Prone organic matter. In the overall area the Faraghan formation is immature to oil
mature, that in begging to medium of oil generating zone as Tmax maturity parameter. These
samples could have better initial source rock and higher Tmax properties assuming their high level
of maturity. Vitrinite reflectance (%Ro) values is different rang and changed to 1.3% and gas
mature zone in West Aghar. %Ro values maximizing at 1.4% which classified as more mature,
within the gas generating window.
In the study area, Faraghan Fm has been selected for accurate source rock evaluation, as the
kerogen chemical structure investigation. The kerogen chemical structure is related to the
composition of petroleum hydrocarbons generated from the kerogen. Results indicate that all the
samples analyzed are residual kerogens that have almost no oil potential. Phenol is detected in all
rocks, indicating a contribution of woody lignin from higher land plants. For all samples, the above
NSO compounds were minor peaks compared with major aromatic compounds (Naphthalene,
Biphenyl, Anthracene, etc) and aliphatic compounds (n-alkanes and n-alkenes). The following
chemical characteristics is revealed by Py-GC analysis of the Zagros samples.
1- Kerogen of the Farghan Formation is rich in aromatic and poor in aliphatic structure compared
with the other five formations in Paleozoic series. Residual kerogens that have almost no potential
2- Faraghan and Dalan samples show aromatic characteristics. Their original immature kerogen
might be Type 3.
50
COLD TEMPERATE BIOTAS AND GLACIAL CONDITIONS DURING THE
LATE PALEOZOIC ICE AGE (LPIA): NEW TIMING AND BETTER
TEMPERATURES
Runnegar B., Beard A., Ivany L.
Recently published CA-IDTIMS U-Pb ages from numerous levels in the Guadalupian and
Lopingian of eastern Australia have collapsed previously lengthy biostratigraphic zones based on
marine invertebrates and palynomorphs into a few million years at the close of the Permian
(Metcalfe et al., 2015; Nicoll et al., 2015). For example, the youngest eight of 22 brachiopod zones
recognized by Waterhouse and Shi (2013) in eastern Australia and New Zealand are now thought to
occupy as little as ~3 Ma of the latest Lopingian. At the Cisuralian end of the Permian, less progress
has been made and the situation has been complicated by the realization that previously widely
accepted SHRIMP U-Pb ages were based on an unreliable standard (SL13) that has large and
unpredictable uncertainties. In particular, a series of SHRIMP ages from a corehole in the Cranky
Corner Basin of New South Wales played an important role in calibrating early Cisuralian marine
invertebrate and palynostratigraphic zones (Archbold et al., 2004; Facer and Foster, 2003).
Problems with both the geochronology and the lithostratigraphy in the Cranky Corner corehole have
complicated understanding of the Cisuralian timescale.
We are attempting to use the much-revised timescale to investigate the climate history of eastern
Australia during the Late Paleozoic Ice Age (LPIA). Our approach is to recover seasonal
temperatures from oxygen isotope ratios recorded in the thick umbonal regions of Eurydesma shells
(Beard et al., 2015; Ivany and Runnegar, 2010) and to use life-associated geologic indicators of cold
conditions (dropstones, glendonites) to constrain both annual temperatures and isotopic composition
of ocean waters. Our work suggests that conditions in eastern Australian during the LPIA may have
been more analogous to Miocene Antarctica rather than modern Antarctica, at least after the major
meltdown that followed the extreme Gzhelian-Asselian glaciation.
51
LATE DEVONIAN AND EARLY CARBONIFEROUS MIOSPORES AND
ACRITARCHS FROM THE SOUTHERN TABAS BLOCK (ZARAND
REGION), CENTRAL IRAN
Sabbaghiyan H., Aria-Nasab M.
Late Devonian and early Carboniferous miospore and microphytoplankton assemblages are
described for the first time from southern Tabas block (southeast Zarand). The measured section in
this area includes the Bahram and Shishtu formations. Fifty-one miospore species (27 genera) and
16 species of acritarch (11 genera) were recorded from Bahram and Shishtu formations and
assigned to three Assemblage Zones. Assemblage Zone I occurs in the lower part of Bahram
Formation and suggests an Upper Devonian (Frasnian) age. Assemblage zone II, occurring in the
Shushtu 1 member, indicates an Upper Devonian (latest Frasnian-Famennian) age for this interval.
Assemblage zone III, which occurs in the Shushtu 2 member, suggests a lower Mississippian
(Middle Tournaisian) age for this member. The assemblages were compared with coeval miospore
and microphytoplankton records elsewhere in the world. The associated marine
microphytoplankton, accompanied by miospores indicate a nearshore depositional.
52
STABLE SULFUR ISOTOPE VARIATION AND FLUID INCLUSION
STUDIES FROM EPITHERMAL PYRITE – GALENA VEINS AT
SPOOHK AREA (KABUTAR KUH) SE GONABAD, EAST IRAN
Sadeghi L.
The Spoohk exploration area is located in the northern part of Lut Block at Kabutar kuh Zone
southeast of Gonabad area in East Iran. Ore-mineralization and related alterations in the area have
occurred by late stage hydrothermal activities of Kalateh Mian magmatic complex. This complex
intruded the Jurassic Shemshak Formation in Eocene period and has a variable composition from
monzogranite to quartz monzodiorite. Alterations with a NW-SE trend are predominantly composed
of phyllic and silicic types and (often with brecciated textures), are delineated from adjacent units.
Ore-paragenesis occurred in three stages along the brecciated-silicified veins under structural-
chemical controls in the following order: pyrite, chalcopyrite, sphalerite, galena, covellite and
quartz (gangue). Sulphur isotope data from three purified galena samples performed at GG-Hatch
laboratory of Ottawa University in Canada, showed Δ34S range values from 0 to 0.2 with an
average 0f 0.1 (per mill). This isotope ratio of heavy sulfur corresponds to a magmatic origin
comparable to Casapalca and Providecia deposits in Peru. Based on thermometric parameters such
as Th and salinity values from fluid inclusion studies, it is concluded that the fluids of
mineralization processes are of magmatic origin, which were mixed with meteoric waters while
flowing upwards. In this area High Temperature of hydrothermal systems results to be impossible
presence of Hydrocarbon window.
53
CONTRIBUTION TO THE EVOLUTION OF THE NORTHERN
GONDWANA MARGIN IN TURKEY: GEODYNAMIC SIGNIFICANCE
OF THE MIDDLE PERMIAN TO LOWER TRIASSIC SUCCESSIONS IN
THE ANTALYA NAPPES (WESTERN AND CENTRAL TAURIDES)
Şahin N., Altiner D.
Detailed stratigraphic studies on the Middle Permian to Lower Triassic rock successions of the
Antalya Nappes, largely exposed in Olympos, Kesmebogazi and Çürükdag around the town of
Kemer, Barak village to the south of the Egirdir Lake, around Cukurköy and Kizilbag villages to the
northwest of the town of Gündogmus and near the town of Demirtas and areas to the north of the
town of Gazipasa near Alanya, have revealed the presence of two episodic rifting events separated
by a period of tectonic quiescence corresponding to the Lopingian (Wuchiapingian and
Changhsingian) to the earliest Triassic (Griesbachian). The first rifting event occurred in the
Capitanian and produced basaltic volcanic rocks intercalated within the shallow marine fossiliferous
carbonate successions. Vitrophyric basaltic extrusions producing distinct pillows in the Kizilbag
Formation severely dolomitized the associated carbonate rocks. The Lopingian to the lowermost
Triassic (Griesbachian) carbonates representing a tectonic quiescence deposited over the Capitanian
volcanics and the successions of the carbonate platform not affected from the rift volcanism. The
second rifting episode started with an abrupt facies change in the late Griesbachian. The upper
Griesbachian to lower Anisian Akıncibeli Formation consisting of variegated shales, limestones and
volcanics was laid down on the carbonate platform. The stratigraphic gap under the Akincibeli
Formation increased in magnitude when the erosional truncation became more active on the
underlying rocks. This truncation occurred in some areas down into the Capitanian and a
considerable erosional relief occurred on the carbonate platform probably reflecting the intensity of
rifting mechanism. The Triassic rifting affecting the carbonate platform successions of the Antalya
Nappes, recorded initially by the deposition of the Akincibeli Formation, continued by a rapid
subsidence leading to an active volcanism and the deposition of a variety of pelagic sediments
containing sometimes Permian and Triassic blocks and clasts.
54
THERMAL EVOLUTION OF THE HOLY CROSS MOUNTAINS (CENTRAL
POLAND) THROUGH MODELLING OF NEW AND OLD THERMAL
MATURITY INDICATORS OF PALAEOZOIC SEDIMENTARY
SUCCESSIONS
Schito A., Corrado S., Trolese M., Aldega L., Caricchi C., Cirilli S., Spina A.
A reliable assessment of thermal maturity of sedimentary successions is crucial for hydrocarbons
research and hence for evaluation of hydrocarbons generation/expulsion. From thermal models
calibration derives the accurate appraisal of the risk assessment. Thus in order to provide reliable
burial/thermal scenarios, it must be adopted more than one parameter of thermal degradation of
kerogen. This work reviews and integrates available thermal maturity data (Conodont Alteration
Index–CAI; Acritarch Alteration Index–AAI and vitrinite reflectance-VR; graptolite reflectance;
illite (I) content in mixed layers Illite-Smectite (I/S) derived from XR Diffraction; Raman
spectroscopy on organic matter; Palinomorphs Darkness Index -PDI) and re-assesses the source
rock potential by using optical analysis of dispersed organic matter and X-ray diffraction of clay
sized fraction of sediments of an area to the West of the “GoldenBelt”. In this area, namely, Holy
Cross Mountains (HCM), Palaeozoic successions crop out. To constrain burial and thermal models,
we used a multi-method approach coupling organic matter optical analysis and X ray diffraction of
clay-size fraction of sediments.
The HCM are located eastward in the central part of the Trans European Suture Zone (TESZ) and
comprise Palaeozoic sedimentary rocks ranging from Cambrian to Early Carboniferous and are
organized into two different tectonic blocks: the Lysogory region to the North and the Kielce region
(part of the Malopolska massif) to the South.
Maps of themal maturity and thickness distribution together with thermal modelling allowed to
draw a 3D thermal evolution of the Palaeozoic successions and to envisage a substantial difference
between the two tectonic blocks related to a different burial history (different thicknesses).
Furthermore 1D thermal models allowed us to define the onset of gas generation for the Silurian
source rocks of the Łysogóry region and point out that sedimentary burial is the main controlling
factor of the measured levels of thermal maturity.
55
NEW RAMAN PARAMETERS INTEGRATED IN CLASSICAL
PETROLEUM SYSTEM MODELLING TO ASSESS THERMAL
EVOLUTION OF SEDIMENTARY BASINS: FOUR CASE HISTORIES
FROM CENOZOIC, MESOZOIC AND PALEOZOIC SEDIMENTARY
SUCCESSIONS
Schito A., Corrado S., Romano C., Guedes A., Grigo D.
Uncertainties in thermal maturity assessment of organic matter dispersed in sediments can strongly
affect the reliability of reconstruction of thermal evolution of sedimentary basins or influence
negatively decisions in hydrocarbon (HC) exploration. Pitfalls in vitrinite reflectance, the most
successful thermal parameter used to calibrate thermal history, are one of the main cause of such
uncertainties. As a matter of fact, several limitations arise when exploring targets that are devoid of
vitrinite macerals (e.g., Lower Paleozoic rocks) and/or are poor in organic matter content, or when
suppression/retardation phenomena occur in high HI souce rocks or in overpressured sections.
In this work we propose a multimethods approach to assess thermal maturity based on indicators
carried out from the analyses on both the organic (e.g. Pyrolysis Rock Eval, Fourier Transform
Infrared Spectroscopy and Raman spectroscopy) and the inorganic (e.g. clay mineralogy, low-
temperature thermochronology) fraction of sediments.
In this work we tested four different case histories in order to analyse Cenozoic, Mesozoic and
Paleozoic source rocks.
Thermal modelling calibrated with classical parameters (from FT-IR, organic petrography,
pyrolysis and XRD on clays) allow us to test and correlate totally new parameters derived from
Raman spectroscopic analyses on the organic fraction of sediments with different levels of
hydrocarbon generation.
Raman investigation on kerogen for thermal maturity assessment turned out to be a powerful tool
because it:
- is not time-consuming;
- can be performed on bulk kerogen or directly on plugs prepared for organic petrography;
- provides an insight on the short-order range chemical processes and thus can provide a
quantitative assessment on the structural changes that can occur during thermal maturation of
kerogen.
Our results demonstrate, for the first time, that Raman spectra of undifferentiated Cenozoic,
Mesozoic and Paleozoic organic matter dispersed in sediments (excluded macerals of the inertinite
group) show quantifiable changes in response to thermal maturation and can be successfully used to
parameterize thermal evolution of source rocks, even at very low diagenetic stages, between the
immature and mid mature stages of hydrocarbon generation. In particular, two successful
parameterizations against vitrinite reflectance are presented in this work, based on the area or width
ratio of the bands that compose Raman spectra. In conclusion variations in the Raman spectra of
kerogen in diagenesis are ruled by completely different mechanisms with respect to those that
occurs during graphitization at higher temperatures in metamorphism.
56
LOWER PALEOZOIC PALY IN ZAGROS, PROSPECTIVITY AND
CHALLENGES
Soleimany B.
Zagros fold and thrust belt is one of the most prolific hydrocarbon provinces in the world with more
than 100 years of exploration history. During the early years of the twentieth century, the first
successful oil discovery in MIS-1 proved oil in the Oilgo-Miocene limestone of the Asmari
Formation.For more than 40 years, all of the discoveries and productions were from theAsmari
reservoir. In 1950’s a new reservoir horizon has been discovered in the Middle Cretaceous
limestone (Bangestan Group). Discovery of the Kangan giant gas field was an important discovery
of gas and condensate accumulation in Triassic and Permian reservoirs (Dehram Group) which
carried out in 1972. No commercial field had been discovered in Iran in the Triassic-Permian before
that. Subsequent exploration drilling in Triassic-Permian reservoirs gave rise to discovery of other
Iranian onshore-offshore giant gas fields in this reservoir level
Since the 1980s testing the new petroleum sourcing theories, including the Paleozoic potentials,
resulted in interesting developments in Oman (The Paleozoic units are older than the Khuff)
moreover, important Paleozoic reservoirs have been discovered in the central Riyadh. In the Zagros
fold and thrust belt few attempts which have been made to test the prospectively of lower Paleozoic
successions during this time period were not successful.
During recent years exploration drilling in the Early Permian Fraghun formation using new
geological concepts lead to discovery of the new petroleum system in the Paleozoic units (older
than the Dalan) in the Zagros fold and thrust belt and offshore Persian Gulf and opened a new
season of exploration in this frontier paly. However it should be considered that the exploring for
Paleozoic deep target is technically challenging in terms of visualization and drilling.
57
APPLICATION OF PALYNOMORPH DARKNESS INDEX (PDI) AND
MICROSPECTROSCOPY TO ASSESS THERMAL MATURITY AND
ASSOCIATED CHANGES IN CHEMISTRY OF PALYNOMORPHS: A
CASE STUDY FROM NORTH AFRICA.
Spina A., Marcogiuseppe A., Cirilli S., Rettori R., Di Michele A., Sassi P., Vecoli M., Riboulleau
A., Servais T.
Organic-walled microfossils can be successfully used in a wide range of geological disciplines other
than biostratigraphy, that include sediment provenance analysis, structural geology, geo-
thermometry and hydrocarbon potential assessment of organic matter. This study focuses on the
thermal maturity assessment of Silurian-Devonian sediments from the Ghadames Basin, North
Africa and is based on optical and microspectroscopic analysis of palynomorphs. In southern
Tunisia, the investigated subsurface cored section comprises the Argiles Principales Formation
spanning an early (Llandovery) to late Silurian age (Ludlow; Vecoli et al., 2009). In Libya, the
studied succession covers the Aouinet Ouenine IV Formation attributed to the Late Devonian
(Frasnian-Famennian).
Geochemical approaches used to reconstruct thermal alteration of sediments necessitate advanced,
relatively expensive analytical techniques. In this study, the fidelity of less costly, relatively simple
approaches of visually assessing palynomorph color to determine thermal alteration (i.e., SCI:
Spore Color Index, TAI: Thermal Alteration Index - Staplin, 1969, and PDI: Palynomorph
Darkness Index, Goodhue and Clayton, 2010) was evaluated.
SCI and TAI are qualitative methods, strictly linked to the operator perception, which uses ten and
five point scales respectively, to characterize color in terms of illustrated specimens and/or
descriptions. In contrast, PDI is obtained from the measurement of the red, green and blue (RGB)
intensities of light transmitted through palynomorphs, using standard optical microscopes and
digital cameras.
The palynomorph-based thermal alteration estimates were compared to FTIR (Fourier Transform
Infrared) analysis and Rock-Eval Pyrolisys data from the same samples. This calibration showed a
linear relationship between these quantitative parameters and the PDI.
These results show that PDI is more reliable than SCI and TAI methods over a wide
paleotemperature range, confirming early results from Goodhue and Clayton (2010).
The next step of this research will be to calibrate PDI with quantitative analysis from other
sedimentary successions to obtain a more rigorous algorithm to underpin development of the
advanced image processing methods that would enable a more quantitative and objective
determination of the organic matter thermal maturity.
58
GONDWANAN PALAEOZOIC PLANT SPORES: A REVIEW
Steemans P., Gerrienne P.
The earliest plant spores are called cryptospores because they are devoid of haptotypic features such
as trilete or monolete mark. They were presumably produced by bryophytes. The earliest
unambiguous cryptospores known to date appear during the Dapingian on the Western Gondwana.
It has however to be noted that some authors consider that some Cambrian palynomorphs are also
cryptospores. The Dapingian and Darriwilian cryptospores are poorly diversified. During the
Sandbian, new morphologies evolve, including specimens enclosed in a membrane. The
assemblages remain stable up to the Aeronian, which suggests that plants had a low evolutionary
rate during more than 22 Myr. Surprisingly, the Hirnantian glaciation did not affect the cryptospore
biodiversity. This putative climatic tolerance may explain why cryptospore-producing plants
survived in latitudes ranging from the palaeoequator up to the palaeopole. The earliest trilete spores
are known from the Katian and the Hirnantian of Saudi Arabia. They were presumably produced by
tracheophytes. They remain very rare up to the Wenlock. Few elements may be used for
biostratigraphy. The main element allowing an estimation of the age is the abundance (i) of trilete
spores and (ii) of cryptospores enclosed in a membrane. The first appearance of the trilete spore
Archaeozonotriletes chulus in the Telychian is the first reliable biostratigraphic event.
From Wenlock times onwards, the palynostratigraphic scheme is better resolved. Palaeogeographic
interpretations become possible. For example, Emphanisporites splendens is only known in the
Ludlow/Pridoli of Gondwana and Spain; Streelispora newportensis is only known in the
Lochkovian of Laurussia and Spain. This strongly suggests that the Iberian plate was located
between Gondwana and Laurussia, and favours plate reconstructions showing a short distance
between the two palaeocontinents.
We described a phylogenetic succession of trilete spores from a Lochkovian to Pragian locality on
the ORSC. Those trilete spores are unknown on the Gondwana, except on the small Moesian peri-
Gondwanian terrane. This terrane has supposedly moved northwards during the Devonian and
collided with Laurussia during Carboniferous times. Our results suggest that the terrane was already
close to the ORSC during Early Devonian times.
The acquisition of the heterospory is the next important step in the evolution of the vegetation.
Heterospory is marked by the development of spores larger than ca. 150 µm. They are called
megaspores and develop into female gametophytes. The microspores are the smaller spores that
develop into male gametophytes. The joint presence of both types of spores is necessary to allow
heterosporous plants to reproduce. A rich, exquisitely preserved assemblage of megaspores has
been described from the Eifelian and the Givetian from Gondwana. Among 20 different taxa of
megaspores, 6 are also known from the Laurussia continent. Their presence on both continents
suggests that they could be transported from one palaeocontinent to the other. In addition, because
(i) large megaspores cannot be transported over long distances, and (ii) megaspores and
microspores need to fall down close to each other, palaeogeographic reconstructions showing a pre-
Pangea during the second half of Devonian are again preferred to reconstructions showing a large
ocean between Laurussia and Gondwana.
59
PERMIAN PALYNOSTRATIGRAPHY: PROGRESS AND CHALLENGES
FOR THE NEXT CENTURY
Stephenson M.
Palynostratigraphy (the use of palynomorphs in biostratigraphy) aims to correlate sedimentary
rocks, and to relate geological resources or events to each other and to other important geological or
scientific phenomena. In the Permian, palynostratigraphy has been used primarily to correlate coal-
and hydrocarbon-bearing rocks within basins and between basins, sometimes at high levels of
biostratigraphic resolution. Though these palynostratigraphic schemes related to resource extraction
have been very successful, their main shortcoming has been a lack of correlation with schemes
outside the basins, coalfields and hydrocarbon fields that they serve, and chiefly a lack of
correlation with the international Permian scale. The benefits of a better integrated general
palynostratigraphy are very great scientifically because there are numerous events of global
scientific interest in the Permian, for example the timing and order of deglaciation events and the
detailed characteristics and timing of mass extinction events within the Permian and at the Permian-
Triassic boundary. Permian palynostratigraphy is strongly affected by phytogeographic
provinciality particularly from the Middle Permian onwards, as predicted by palaeobotanical
studies. This makes correlation between regional palynostratigraphic schemes difficult. For these
reasons it is unlikely that a single comprehensive palynostratigraphic scheme for the Permian
globally will ever be developed. However local high resolution palynostratigraphic schemes for
regions are being linked either by precise assemblage level quantitative taxonomic comparison or
by the use of single well-characterised palynological taxa that occur across Permian
phytogeographical provinces. Such taxa include: Scutasporites spp., Vittatina spp., Weylandites
spp., Lueckisporites virkkiae, Otynisporites eotriassicus and Converrucosisporites confluens. These
palynological correlations can be facilitated and supplemented with radiometric,
magnetostratigraphic, independent faunal, and strontium isotopic dating. None of the Permian
GSSPs involve palynological definitions, which may be problematic given the importance of
palynology in correlation in the commercial and academic worlds. However there appear to be taxa
that occur at GSSPs or well-dated boundary sections that could be used to correlate those
boundaries. For example Aratrisporites and Otynisporites eotriassicus may be useful to correlate
the Permian-Triassic boundary into non-marine sections or sections without radiometric dates.
Converrucosisporites confluens may be useful in correlating the Carboniferous-Permian boundary.
60
PALYNOLOGICAL ASSEMBLAGES ACROSS THE HERCYNIAN
UNCONFORMITY IN WESTERN IRAQ
Stephenson M., Al-Mashaikie S.
Recent study of samples from borehole KH-5/1 has allowed an assessment of the duration of the
hiatus associated with the so-called Hercynian unconformity (also known as the ‘Late
Carboniferous unconformity’ or ‘pre-Unayzah unconformity’) in western Iraq. KH-5/1 was drilled
as a deep water well and fully cored to TD at 1620m. The well section spans the unconformity at
670m depth with the Raha Formation below and the Ga’ara Formation above. The unconformity
appears to be associated with non-deposition or erosion of rocks corresponding approximately in
age to part of the Serpukhovian and Bashkirian (latest Mississippian to early Pennsylvanian),
similar to the duration associated with the same unconformity in well ST-8 situated to the south of
KH-5/1 in northern Saudi Arabia.
The Ga’ara Formation assemblages above the unconformity in KH-5/1 are similar in character to
those described from 4620 to 4200 feet in ST-8. The age of these assemblages in both KH-5/1 and
ST-8 is considered in this paper to be Westphalian. The composition of the Ga’ara Formation
assemblages in KH-5/1 also shows some similarity to glacigene post-unconformity beds of the 2165
Biozone of the Al Khlata Formation of Oman.
61
SELECTED SPORES AND POLLEN FROM THE PERMIAN UMM IRNA
FORMATION, JORDAN, AND THEIR STRATIGRAPHIC UTILITY IN
THE MIDDLE EAST AND NORTH AFRICA
Stephenson M., Powell J.
The Umm Irna Formation, exposed along the eastern shore of the Dead Sea, has been the focus of
intense palaeobotanical study, but more recently it has been revealed that well preserved
palynological assemblages are also present. The age of the Umm Irna Formation is such that it
provides a showcase for taxa from the Mid to Late Permian which are hard to find in the carbonate-
dominated successions to the southeast in the Arabian Peninsula and elsewhere in the Middle East.
In this paper distinctive taxa present in the Umm Irna Formation are described and illustrated, and
surveyed for their stratigraphic occurrences, to consider their suitability for biozonal indices within
the Mid to early Late Permian. Two appear to be promising: Protohaploxypinus uttingii Stephenson
and Filatoff, 2000 and Pretricolpipollenites bharadwaji Balme, 1970. The first is distinctive in that
it is relatively small, has numerous, very narrow taenaie, and a shrunken intexinal corpus; the
second has three narrow distal sulci. Both taxa may have first appearance levels within the Permian
above the base of the OSPZ6 palynological Biozone, and thus may be useful in the future for further
biozonation.
62
NEW TAXONOMICAL AND PALAEOGEOGRAPICAL DATA OF SMALLER
TETHYAN FORAMINIFERS
Vachard D.
New data are provided about the biostratigraphy of Permian smaller foraminifers belonging to four
classes: Fusulinata, Miliolata, Nodosariata, and Textulariata. Biomarkers are principally known in
the orders and superfamilies, Lasiodiscoidea, Bradyinoidea and Globivalvulinoidea (Fusulinata),
Cornuspirida (Miliolata), and in the whole class of the Nodosariata. The class Textulariata is too
little known during the Permian to play currently a significant biostratigraphic role; nevertheless,
the appearance of the order Ataxophragmiida is probably an important bioevent. The main genera
among the lasiodiscids are Mesolasiodiscus, Lasiodiscus, Pseudovidalina, Xingshandiscus; the
bradyinoids Bradyina and Postendothyra; the globivalvulinoids Globivalvulina,
Septoglobivalvulina, Labioglobivalvulina, Paraglobivalvulina, Sengoerina, Dagmarita, Danielita,
Louisettita, Paradagmarita, Paradagmaritopsis and Paremiratella; the miliolates Rectogordius,
Okimuraites, Glomomidiella, Neodiscus, Multidiscus, Hemigordiopsis, Lysites, Shanita and
Glomomidiellopsis. The discussed Nodosariata are Nodosinelloides, Tezaquina, Polarisella,
Geinitzina, Pachyphloia, Rectoglandulina, first true Nodosaria, Langella, Pseudolangella,
Calvezina, Cryptoseptida, Wanganella, Colaniella, Frondina, and Ichthyofrondina, but their
complete lineages are too poorly understood to permit an accurate biostratigraphical use for the
moment. Finally, palaeobiogeographical implications of lasiodiscoids and globivalvulinoids, as well
as the genera Shanita and Colaniella are given.
63
ANGELITA (FORAMINIFERA, PSEUDOVIDALINIDAE), AS A MARKER OF
THE OPENING OF NEOTETHYS DURING THE MIDDLE-LATE
PERMIAN
Vachard D., Rettori R., Altıner D., Gennari V., Grigoryan G., Zambetakkis A., Ghazzay W.,
Razgallah S., Ghorbani M., Kani A., Aria-Nasab M., Sabbaghian H., Keyvan Z.
Angelina is sometimes considered as a junior synonym of Xingshandiscus. This synonymy is
irrelevant, because Angelina is unilayered pseudofibrous, whereas Xingshandiscus exhibits a
bilayered wall, dark microgranular and clear pseudofibrous. Moreover, as Angelina is a pre-
occupied name, Angelita nom. nov. is proposed to replace it. Angelita reveals the most advanced
evolutionary stage of pseudovidalinid foraminifers. The parallel evolution of lasiodiscoids and
archaediscoids is again verified, since the evolved lasiodiscoid Angelita is a homeomorph of the
evolved archaediscid Browneidiscus. This remarkable homeomorphy of both groups (with the same
stages, involutus, concavus, angulatus and tenuis) explains some serious mistakes with so-called
Late Carboniferous-Early Permian archaediscids, which belong in reality to lasiodiscids. Angelita
was first discovered in the Taurus Mountains of southern Turkey; then, in Armenia. During
numerous investigations in the Permian limestones, we newly discovered Angelita in Chios Island
(Greece), Abadeh (central Iran), and Jebel Tebaga (Tunisia). Other citations of Angelita, for
example in Hungary, are not acceptable, due to confusions with cornuspirids or other miliolate
foraminifers. As Angelita is a shallow stenobath and tropical stenotherm devoid of planktonic larval
stages, its distribution permits to demonstrate the geographic and climatic continuity and
homogeneity of the carbonate platforms where it lived. Therefore, this continue Peri-Gondwanan
margin platform is described here as the Angelita Province in the western Tethys. However, it is
rapidly separated from Peri-Gondwana, and migrates up to the Cimmerian terranes, as opening of
the Neotethys increased, at the end of Permian and/or at the beginning of Triassic. In contrast to
other palaeobiogeographic foraminiferal markers, like Eopolydiexodina, Rugososchwagerina or
Shanita, it seems that Angelita is only distributed from Tunisia to Iran, but lacks in central
Afghanistan, Tibet, western Myanmar and western Thailand, because these eastern blocks and
terranes were first separated from the Gondwana, and integrated among the Cimmerian terranes.
64
EARLY TRIASSIC FAUNA (MAINLY FORAMINIFERS) FROM CAUCASUS
AND GORNY MANGYSHLAK
Vuks V. J.
Early Triassic microfauna of the Gorny Mangyshlak and Eastern Precaucasus mainly represented by
foraminifers and conodonts. These foraminifer assemblages of Caucasus area and Gorny
Mangyshlak have some typical features: nodosariids are very diverse, attached and primitive
agglutinated foraminifers dominate by quantity of examples. In the first territory, the foraminifer
and conodont assemblages occur in the upper Olenekian. Besides mentioned microfauna, the upper
Olenekian (the Columbites beds) contains abundant recrystallized microgastropods and ostracods.
In the second territory, the mentioned microfaunal groups are in the Olenekian. The richest and
various faunal assemblages occur in the Columbites beds of the upper Olenekian. In the Western
Precaucasus (Granichnaya 16 well) there are poor foraminifer assemblage with attached and
primitive agglutinated foraminifers, and rare nodosariids and miliolids. This assemblage
corresponds to the Olenekian – Anisian conditionally. The maximal diverse and rich faunal groups
of the Gorny Mangyshlak, Eastern Precaucasus and may be Western Precaucasus correspond to the
Late Olenekian time and they indicate more favorable paleoenvironmental conditions in this time.
There are foraminifers and some conodonts in the Lower Triassic of the Western Caucasus.
Foraminifer assemblages correlate to the upper Induan and lower Olenekian. The maximal variety
of the faunal assemblages corresponds to the Early Olenekian time. It marks those more favorable
conditions for the Western Caucasus marine fauna was at this time. Besides, foraminifer
assemblage of the uppermost Induan to the lower part of the upper Olenekian of Crimea consists of
nodosariids are very diverse, attached and primitive agglutinated foraminifers and contains
Meandrospira.
Widely distributed species of foraminifers, conodonts, and ammonoids sometimes occur in the
Lower Triassic of the mentioned regions. Therefore, it is possible to correlate the Lower Triassic
(especially Olenekian) of the Gorny Mangyshlak to coeval deposits of Eastern Precaucasus, and
Western Caucasus, and to the global stratigraphic scale. The study of the taxonomic composition of
the Early Triassic foraminifer assemblages from these regions allows us to mark that these
communities are close to the coeval foraminifer assemblages from the some areas of the
Carpathians and Balkans. The Olenekian transgression makes the more favorable conditions for
foraminifers and to cultivate the similar communities on the discussed territories.
The Peri-Tethys Program, PALSIRP-Sepkoski Grant (USA) and the Cariplo Foundation and
Landau Network - Centro Volta (Italy) supported this research, at different times. This work is a
contribution to the IGCP 630.
65
Al-Mashaikie S. - Department of Geology, College of Sciences, University of Baghdad, Al-
Jadriyah, Al-Karadah, Baghdad, Iraq. E-mail: [email protected]
Alavi Taleghani E. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Aldega L. – Department of Earth Sciences, Roma Sapienza University, Rome, Italy. E-mail:
Altiner D. - Department of Geological Engineering, Middle East Technical University, Ankara,
Turkey. E-mail: [email protected]
Angiolini L. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:
Aria-Nasab M. - Kharazmi University and Exploration Directorate of National Iranian Oil
Company (NIOCEXP), Tehran, Iran. E-mail: [email protected]
Asghari A. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Asilian Mahabadi H. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Atasoy S. G. - Middle East Technical University, Department of Geological Engineering, Ankara,
Turkey. E-mail: [email protected]
Bagnoli G. - Department of Earth Sciences, University of Pisa, Italy. E-mail:
Bahrammanesh Tehrani M. - Geological Survey of Iran, Tehran, Iran. E-mail:
Balini M. - Department of Earth Sciences "A. Desio”, University of Milano, Italy. E-mail:
Barrier E. - Pierre et Marie Curie University (UPMC), National Center for Scientific Research
(CNRS), Paris, France. E-mail: [email protected]
Baud A. - BCG, Lausanne, Switzerland. E-mail: [email protected]
Beard A. - University of Connecticut, Storrs, USA. E-mail: [email protected]
Bergomi M. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.
Bernardi M. - MUSE – Science Museum, Trento, Italy. E-mail: [email protected]
Berra F. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:
Borlenghi L. M. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.
Brenckle P. L. - Consultant, Westport, USA. E-mail: [email protected]
Breuer P. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,
Dhahran, Saudi Arabia. E-mail: [email protected]
Brocke R. - Senckenberg Research Institute and Natural History Museum, Department of
Palaeontology and Historical Geology, Frankfurt an Main, Germany. E-mail:
Broutin J. - Pierre et Marie Curie University (UPMC), Paris, France. E-mail: [email protected]
Bussert R. - Technical University of Berlin, Institute for Applied Geo-sciences, Department of
Exploration Geology, Berlin, Germany. E-mail: [email protected]
66
Caricchi C. - INGV, Rome, Italy. E-mail: [email protected]
Cirilli S. - Department of Physics and Geology, University of Perugia, Italy. E-mail:
Clayton G. - Center for Palynology, Department of Animal and Plant Sciences, University of
Sheffield, United Kingdom. E-mail: [email protected]
Collins J. F. - ExxonMobil Development Company, Spring, USA. E-mail:
Corrado S. - University of Roma Tre, Department of Geological Sciences Rome, Italy. E-mail:
Crasquin S. - Pierre et Marie Curie University (UPMC), Paris, France. E-mail:
Daneshian J. - Kharazmi University, Tehran, Iran. E-mail: [email protected]
Daryabandeh M. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Di Michele A. - Department of Physics and Geology, University of Perugia, Italy. E-mail:
Eidani M. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran. E-mail:
Farahani M. - Rega Zamin Sakht Consulting Co., Tehran, Iran. E-mail:
Fazli L. - Department of Geology, Damavand Branch, Islamic Azad University, Tehran, Iran. E-
mail: [email protected]
Gaetani M. - University of Milano, Italy. E-mail: [email protected]
Gaillot J. - Department of Biostratigraphy, Total, Pau, France. E-mail: [email protected]
Garbelli C. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy, and Nanjing
Institute of Geology and Palaeontology, Chinese Academy of Sciences, Nanjing, Jiangsu, China. E-
mail: [email protected]
Gennari V. - Department of Physics and Geology, University of Perugia, Italy. E-mail:
Gerrienne P. - University of Liège, Belgium. E-mail: [email protected]
Ghalamghash J. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran.
E-mail: [email protected]
Ghazzay W. - Department of Geology, Faculty of Sciences, University of Tunis, Tunisia. E-mail:
Ghorbani M. - Department of Geology, Faculty of Geoscience, Shahid Beheshti University and
Arian Zamin Co.,Tehran, Iran. E-mail: [email protected]
Gómez Cruz A. - University of Caldas, Manizales, Colombia. E-mail:
Grigo D. - ENI spa - Exploration & Production Division, San Donato Milanese, Milan, Italy. E-
mail: [email protected]
Grigoryan G. - Smbat Zoravar street, building 40, apt. 1, Yerevan, Armenia. E-mail:
Guedes A. - University of Porto, Portugal. E-mail: [email protected]
67
Haghighat N. - Department of Geology, Faculty of Science, Kharazmi University, Tehran, Iran. E-
mail: [email protected]
Haig D. W. - Centre for Energy Geoscience, School of Earth & Environment, The University of
Western Australia, Crawley, Australia. E-mail: [email protected]
Hajian M. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail: [email protected]
Hamdi B. - Scientific Board of Research Institute of Earth Science, Geological Survey of Iran,
Tehran, Iran. E-mail: [email protected]
Hasan Goodarzi M. G. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Hassan Kermandji A. - University of Constantine 1, Constantine, Algeria. E-mail:
Heidarzadeh G. - Geological Survey of Iran, Tehran, Iran.
Hooker N. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,
Dhahran, Saudi Arabia. E-mail: [email protected]
Ivany L. - Syracuse University, NY, USA. E-mail: [email protected]
Jäger H. - GeoResources Steinbeis-TransferCentre, Heidelberg, Germany. E-mail:
Kani A. - Department of Geology, Faculty of Geoscience, Shahid Beheshti Univesity, Tehran, Iran.
E-mail: [email protected]
Kavoosi M.A. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran,
Iran. E-mail: [email protected]
Keyvan Z. - Department of Geology, Faculty of Geoscience, Shahid Beheshti University, Tehran,
Iran.
Khelifi Touhami F. - University of Constantine 1, Constantine, Algeria. E-mail:
Krystyn L. - Institute of Palaeontology, Geocenter University Vienna, Austria. E-mail:
Lemus-Restrepo A. - University of Caldas, Manizales, Colombia. E-mail:
Lotfi M. - Azad Islamic University, Tehran, Iran. E-mail: [email protected]
Machado G. - ChronoSurveys Stratigraphic Consultants, Almada, Portugal. E-mail:
Mandrioli R. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.
Marcogiuseppe A. - Department of Physics and Geology, University of Perugia, Italy. E-mail:
Marjibi S. - Petroleum Development Oman, Muscat, Sultanate of Oman. E-mail:
Mazaheri Johari M. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran,
Iran. E-mail: [email protected]
Moezzi Nasab R. - Sistan and Baluchestan University, Daneshgah, Iran. E-mail:
Mohamadi M. - Payame Noor University, Tehran, Iran. E-mail: [email protected]
68
Moradi M. - Zarmesh Mining Group, Tehran, Iran. E-mail: [email protected]
Moreno-Sánchez M. - University of Caldas, Manizales, Colombia. E-mail:
Mory A.J. - Geological Survey of Western Australia, Perth, Western Australia. E-mail:
Motamedi H. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Nicora A. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:
Ökzan Altiner S. - Middle East Technical University, Department of Geological Engineering,
Ankara, Turkey. E-mail: [email protected]
Petti F.M. - MUSE – Science Museum, Trento, Italy. E-mail: [email protected]
Piryaei A. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail: [email protected]
Powell J. - British Geological Survey, Keyworth, Nottingham, England, United Kingdom. E-mail:
Pur Nourbakhsh F. - Geological Survey of Iran, Tehran, Iran. E-mail: [email protected]
Rashidi M. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran, Iran.
E-mail: [email protected]
Razgallah S. - Department of Geology, Faculty of Sciences, University of Tunis, Tunis, Tunisia. E-
mail: [email protected]
Rettori R. - Department of Physics and Geology, University of Perugia, Italy E-mail:
Rezaie Rad A. - Atila Orthoped Company, Tehran, Iran. E-mail: [email protected]
Rezaiparto K. - Department of Geology, Damavand Branch, Islamic Azad University, Tehran,
Iran. E-mail: [email protected]
Riboulleau A. - Laboratoire d'Océanologie et de Géosciences (LOG) UMR CNRS 8187, UFR de
Sciences de la Terre, Lille, France. E-mail: [email protected]
Richoz S. - University of Graz, Institute for Earth Sciences, Graz, Austria. E-mail:
Romano C. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:
Runnegar B. - University of California, Los Angeles, USA. E-mail: [email protected]
Sabbaghiyan H. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran,
Iran. E-mail: [email protected]
Sadeghi L. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran. E-mail:
Saeidi A. - Rega Zamin Sakht Consulting Co., Tehran, Iran. E-mail: [email protected]
Şahin N. - Turkish Petroleum, Ankara, Turkey. E-mail: [email protected]
Sassi P. - Department of Chemistry, Biology and Biotechnology, University of Perugia, Italy. E-
mail: [email protected]
Schito A. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:
69
Servais T. - Unité EVO ECO PALEO - Evolution, Ecologie et Paléontologie - UMR CNRS 8198,
UFR des Sciences de la Terre, Lille, France. E-mail: [email protected]
Shamani F. - Ministry of Energy, Water Resources of the Semnan Province, Garmsar, Iran. E-mail:
Sohrabi Z. - Geological Survey of Iran, Tehran, Iran.
Soleimany B. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:
Spina A. - Department of Physics and Geology, University of Perugia, Italy. E-mail:
Steemans P. - University of Liège, Belgium. E-mail: [email protected]
Stephenson M. - British Geological Survey, Keyworth, Nottingham, England, United Kingdom. E-
mail: [email protected]
Tahmasebi Sarvestani A. - Exploration Directorate of National Iranian Oil Company (NIOCEXP),
Tehran, Iran. E-mail: [email protected]
Trolese M. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:
Tsuchida K. - Japan Oil, Gas and Metals National Corporation (JOGMEC), Japan. E-mail:
Vachard D. - University of Science and Technology of Lille, France. E-mail:
Vavrdova M. - Institute of Geology, Academy of Science of the Czech Republic, Praha, Czech
Republic. E-mail: [email protected]
Vecoli M. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,
Dhahran, Saudi Arabia. E-mail: [email protected]
Vennin E. - University of Burgundy, Dijon, France. E-mail: [email protected]
Vuks V.J. - A.P. Karpinsky Russian Geological Research Institute, (FGBU “VSEGEI”), St.
Petersburg, Russia. E-mail: [email protected]
Vuolo I. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.
Zambetakkis A. - Department of Geology and Geoenvironments, University of Athens, Greece. E-
mail: [email protected]
Zanchetta S. - Department of Earth and Environmental Sciences, University of Milano-Bicocca,
Italy. E-mail: [email protected]
Zanchi A. - Department of Earth and Environmental Sciences, University of Milano-Bicocca, Italy.