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: geozakee13@yahoo.com

Alavi Taleghani E. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

e.taleghani@yahoo.com

Aldega L. – Department of Earth Sciences, Roma Sapienza University, Rome, Italy. E-mail:

luca.aldega@uniroma1.it

Altiner D. - Department of Geological Engineering, Middle East Technical University, Ankara,

Turkey. E-mail: demir@metu.edu.tr

Angiolini L. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:

lucia.angiolini@unimi.it

Aria-Nasab M. - Kharazmi University and Exploration Directorate of National Iranian Oil

Company (NIOCEXP), Tehran, Iran. E-mail: mohammadrtk@gmail.com

Asghari A. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

afshin_asghari@yahoo.com

Asilian Mahabadi H. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

hosseinasilian@yahoo.com

Atasoy S. G. - Middle East Technical University, Department of Geological Engineering, Ankara,

Turkey. E-mail: satasoy@metu.edu.tr

Bagnoli G. - Department of Earth Sciences, University of Pisa, Italy. E-mail:

gabriella.bagnoli@unipi.it

Bahrammanesh Tehrani M. - Geological Survey of Iran, Tehran, Iran. E-mail:

bahrammanesh69@gmail.com

Balini M. - Department of Earth Sciences "A. Desio”, University of Milano, Italy. E-mail:

marco.balini@unimi.it

Barrier E. - Pierre et Marie Curie University (UPMC), National Center for Scientific Research

(CNRS), Paris, France. E-mail: eric.barrier@upmc.fr

Baud A. - BCG, Lausanne, Switzerland. E-mail: aymon.baud@unil.ch

Beard A. - University of Connecticut, Storrs, USA. E-mail: jamesandrewbeard@gmail.com

Bergomi M. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.

Bernardi M. - MUSE – Science Museum, Trento, Italy. E-mail: massimo.bernardi@muse.it

Berra F. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:

fabrizio.berra@unimi.it

Borlenghi L. M. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy.

Brenckle P. L. - Consultant, Westport, USA. E-mail: saltwaterfarm1@gmail.com

Breuer P. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,

Dhahran, Saudi Arabia. E-mail: pierre.breuer@aramco.com

Brocke R. - Senckenberg Research Institute and Natural History Museum, Department of

Palaeontology and Historical Geology, Frankfurt an Main, Germany. E-mail:

rainer.brocke@senckenberg.de

Broutin J. - Pierre et Marie Curie University (UPMC), Paris, France. E-mail: jean.broutin@upmc.fr

Bussert R. - Technical University of Berlin, Institute for Applied Geo-sciences, Department of

Exploration Geology, Berlin, Germany. E-mail: r.bussert@tu-berlin.de

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Caricchi C. - INGV, Rome, Italy. E-mail: chiara.caricchi@uniroma3.it

Cirilli S. - Department of Physics and Geology, University of Perugia, Italy. E-mail:

simonetta.cirilli@unipg.it

Clayton G. - Center for Palynology, Department of Animal and Plant Sciences, University of

Sheffield, United Kingdom. E-mail: gclayton@tcd.ie

Collins J. F. - ExxonMobil Development Company, Spring, USA. E-mail:

joel.f.collins@exxonmobil.com

Corrado S. - University of Roma Tre, Department of Geological Sciences Rome, Italy. E-mail:

sveva.corrado@uniroma3.it

Crasquin S. - Pierre et Marie Curie University (UPMC), Paris, France. E-mail:

sylvie.crasquin@upmc.fr

Daneshian J. - Kharazmi University, Tehran, Iran. E-mail: daneshian@tmu.ac.ir

Daryabandeh M. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

mdaryabandeh@yahoo.com

Di Michele A. - Department of Physics and Geology, University of Perugia, Italy. E-mail:

alessandro.dimichele@unipg.it

Eidani M. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran. E-mail:

m.eidani71@gmail.com

Farahani M. - Rega Zamin Sakht Consulting Co., Tehran, Iran. E-mail:

mostafa_khoshduni@yahoo.com

Fazli L. - Department of Geology, Damavand Branch, Islamic Azad University, Tehran, Iran. E-

mail: fazli52@yahoo.com

Gaetani M. - University of Milano, Italy. E-mail: maurizio.gaetani@unimi.it

Gaillot J. - Department of Biostratigraphy, Total, Pau, France. E-mail: jeremie.gaillot@total.com

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: claudio.garbelli@nigpas.ac.cn

Gennari V. - Department of Physics and Geology, University of Perugia, Italy. E-mail:

valerio.gennari@studenti.unipg.it

Gerrienne P. - University of Liège, Belgium. E-mail: p.gerrienne@ulg.ac.be

Ghalamghash J. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran.

E-mail: ghalamaghash@yahoo.com

Ghazzay W. - Department of Geology, Faculty of Sciences, University of Tunis, Tunisia. E-mail:

wissalghazzay@yahoo.fr

Ghorbani M. - Department of Geology, Faculty of Geoscience, Shahid Beheshti University and

Arian Zamin Co.,Tehran, Iran. E-mail: m_ghorbani@hotmail.com

Gómez Cruz A. - University of Caldas, Manizales, Colombia. E-mail:

arley.gomez@ucaldas.edu.co

Grigo D. - ENI spa - Exploration & Production Division, San Donato Milanese, Milan, Italy. E-

mail: domenico.grigo@eni.com

Grigoryan G. - Smbat Zoravar street, building 40, apt. 1, Yerevan, Armenia. E-mail:

gevgrigg@mail.ru

Guedes A. - University of Porto, Portugal. E-mail: aguedes@fc.up.pt

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Haghighat N. - Department of Geology, Faculty of Science, Kharazmi University, Tehran, Iran. E-

mail: nooshin_hagh2001@yahoo.com

Haig D. W. - Centre for Energy Geoscience, School of Earth & Environment, The University of

Western Australia, Crawley, Australia. E-mail: david.haig@uwa.edu.au

Hajian M. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail: mah_hajian@yahoo.com

Hamdi B. - Scientific Board of Research Institute of Earth Science, Geological Survey of Iran,

Tehran, Iran. E-mail: hbahaedin@yahoo.com

Hasan Goodarzi M. G. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

hgoodarzigeo@yahoo.com

Hassan Kermandji A. - University of Constantine 1, Constantine, Algeria. E-mail:

adnankermandji@yahoo.com

Heidarzadeh G. - Geological Survey of Iran, Tehran, Iran.

Hooker N. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,

Dhahran, Saudi Arabia. E-mail: nigel.hooker@aramco.com

Ivany L. - Syracuse University, NY, USA. E-mail: lcivany@syr.edu

Jäger H. - GeoResources Steinbeis-TransferCentre, Heidelberg, Germany. E-mail:

jaeger@georesources.de

Kani A. - Department of Geology, Faculty of Geoscience, Shahid Beheshti Univesity, Tehran, Iran.

E-mail: anoshiravan.kani@gmail.com

Kavoosi M.A. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran,

Iran. E-mail: m.kavoosi@niocexp.ir

Keyvan Z. - Department of Geology, Faculty of Geoscience, Shahid Beheshti University, Tehran,

Iran.

Khelifi Touhami F. - University of Constantine 1, Constantine, Algeria. E-mail:

khelkifi_t_fatima@yahoo.fr

Krystyn L. - Institute of Palaeontology, Geocenter University Vienna, Austria. E-mail:

leopold.krystyn@univie.ac.at

Lemus-Restrepo A. - University of Caldas, Manizales, Colombia. E-mail:

alexander.lemus@ucaldas.edu.co

Lotfi M. - Azad Islamic University, Tehran, Iran. E-mail: lotfi.m@gmail.com

Machado G. - ChronoSurveys Stratigraphic Consultants, Almada, Portugal. E-mail:

machadogil@gmail.com

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:

nunzio.marcogiuseppe@gmail.com

Marjibi S. - Petroleum Development Oman, Muscat, Sultanate of Oman. E-mail:

salmeen.marjibi@pdo.co.om

Mazaheri Johari M. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran,

Iran. E-mail: m.mazaheri.pal@gmail.com

Moezzi Nasab R. - Sistan and Baluchestan University, Daneshgah, Iran. E-mail:

reza.m1371@yahoo.com

Mohamadi M. - Payame Noor University, Tehran, Iran. E-mail: mahin.mohamadi@pnu.ac.ir

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Moradi M. - Zarmesh Mining Group, Tehran, Iran. E-mail: mmoradi.geo@gmail.com

Moreno-Sánchez M. - University of Caldas, Manizales, Colombia. E-mail:

mario.moreno@ucaldas.edu.co

Mory A.J. - Geological Survey of Western Australia, Perth, Western Australia. E-mail:

arthur.mory@dmp.wa.gov.au

Motamedi H. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

h_motamedi2000@yahoo.com

Nicora A. - Department of Earth Sciences ‘‘A. Desio’’, University of Milano, Italy. E-mail:

alda.nicora@unimi.it

Ökzan Altiner S. - Middle East Technical University, Department of Geological Engineering,

Ankara, Turkey. E-mail: altiner@metu.edu.tr

Petti F.M. - MUSE – Science Museum, Trento, Italy. E-mail: fabio.petti@muse.it

Piryaei A. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail: piryaei@gmail.com

Powell J. - British Geological Survey, Keyworth, Nottingham, England, United Kingdom. E-mail:

jhp@bgs.ac.uk

Pur Nourbakhsh F. - Geological Survey of Iran, Tehran, Iran. E-mail: rimafaranak@gmail.com

Rashidi M. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran, Iran.

E-mail: mehrab_rashidi@yahoo.com

Razgallah S. - Department of Geology, Faculty of Sciences, University of Tunis, Tunis, Tunisia. E-

mail: wissalghazzay@yahoo.fr

Rettori R. - Department of Physics and Geology, University of Perugia, Italy E-mail:

roberto.rettori@unipg.it

Rezaie Rad A. - Atila Orthoped Company, Tehran, Iran. E-mail: aerf_rezairad@yahoo.com

Rezaiparto K. - Department of Geology, Damavand Branch, Islamic Azad University, Tehran,

Iran. E-mail: krezaeeparto@yahoo.com

Riboulleau A. - Laboratoire d'Océanologie et de Géosciences (LOG) UMR CNRS 8187, UFR de

Sciences de la Terre, Lille, France. E-mail: armelle.riboulleau@univ-lille1.fr

Richoz S. - University of Graz, Institute for Earth Sciences, Graz, Austria. E-mail:

sylvain.richoz@uni-graz.at

Romano C. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:

claudia.romano@uniroma3.it

Runnegar B. - University of California, Los Angeles, USA. E-mail: runnegar@ucla.edu

Sabbaghiyan H. - Exploration Directorate of National Iranian Oil Company (NIOCEXP), Tehran,

Iran. E-mail: h.sabbaghiyan@gmail.com

Sadeghi L. - Research Institute for Earth Sciences, Geological Survey of Iran, Tehran, Iran. E-mail:

lida.sadeghi@gsi.ir

Saeidi A. - Rega Zamin Sakht Consulting Co., Tehran, Iran. E-mail: abdollahsaidi@yahoo.fr

Şahin N. - Turkish Petroleum, Ankara, Turkey. E-mail: nsahin@tp.gov.tr

Sassi P. - Department of Chemistry, Biology and Biotechnology, University of Perugia, Italy. E-

mail: paola.sassi@unipg.it

Schito A. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:

andrea.schito@uniroma3.it

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Servais T. - Unité EVO ECO PALEO - Evolution, Ecologie et Paléontologie - UMR CNRS 8198,

UFR des Sciences de la Terre, Lille, France. E-mail: thomas.servais@univ-lille1.fr

Shamani F. - Ministry of Energy, Water Resources of the Semnan Province, Garmsar, Iran. E-mail:

fa.shamani@yahoo.com

Sohrabi Z. - Geological Survey of Iran, Tehran, Iran.

Soleimany B. - National Iranian Oil Company (NIOC), Tehran, Iran. E-mail:

b_soleimany@yahoo.com

Spina A. - Department of Physics and Geology, University of Perugia, Italy. E-mail:

amalia.spina@unipg.it

Steemans P. - University of Liège, Belgium. E-mail: p.steemans@ulg.ac.be

Stephenson M. - British Geological Survey, Keyworth, Nottingham, England, United Kingdom. E-

mail: mhste@bgs.ac.uk

Tahmasebi Sarvestani A. - Exploration Directorate of National Iranian Oil Company (NIOCEXP),

Tehran, Iran. E-mail: alirezatahmasebi@gmail.com

Trolese M. - University of Roma Tre, Department of Geological Sciences, Rome, Italy. E-mail:

matteo.trolese@uniroma3.it

Tsuchida K. - Japan Oil, Gas and Metals National Corporation (JOGMEC), Japan. E-mail:

tsuchida.kunihiro@jogmec.go.jp

Vachard D. - University of Science and Technology of Lille, France. E-mail:

daniel.vachard@univ-lille1.fr

Vavrdova M. - Institute of Geology, Academy of Science of the Czech Republic, Praha, Czech

Republic. E-mail: vavrdova@gli.cas.cz

Vecoli M. - Biostratigraphy Group, Geological Technical Services Department, Saudi Aramco,

Dhahran, Saudi Arabia. E-mail: marco.vecoli@aramco.com

Vennin E. - University of Burgundy, Dijon, France. E-mail: emmanuelle.vennin@u-bourgogne.fr

Vuks V.J. - A.P. Karpinsky Russian Geological Research Institute, (FGBU “VSEGEI”), St.

Petersburg, Russia. E-mail: Valery_Vuks@vsegei.ru

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: zambetaki@geol.uoa.gr

Zanchetta S. - Department of Earth and Environmental Sciences, University of Milano-Bicocca,

Italy. E-mail: stefano.zanchetta@unimib.it

Zanchi A. - Department of Earth and Environmental Sciences, University of Milano-Bicocca, Italy.