DYNAMICS and ACTIVE PROCESSES - International Lithosphere ...

6 th WORKSHOP of the ILP TASK FORCE on 

SEDIMENTARY BASINS 

hosted by the Polytechnic University of Tirana (PUTirana) 

DYNAMICS and ACTIVE PROCESSES: 

the ALBANIAN NATURAL LABORATORY 

and ANALOGUES 

ABSTRACT VOLUME and PROGRAMME 

TIRANA, ALBANIA 

November 7- November 12, 2010

Organizing Committee 

Kristaq MUSKA (PUTirana, Albania) 

Shaqir NAZAJ (PUTirana, Albania) 

Liviu MATENCO (VU-Amsterdam, the Netherlands) 

François ROURE (IFP, France) 

Scientific Committee 

Giovanni BERTOTTI (VU-Amsterdam, the Netherlands) 

Salvator BUSHATI (Academy of Sciences, Tirana, Albania) 

Sierd CLOETINGH (VU-Amsterdam, the Netherlands) 

Carlo DOGLIONI (Univ. La Sapienza, Roma, Italy) 

Ilia FILI (Visoka Energy Co., Fieri, Albania) 

Perparim HOXHA (PUTirana, Albania) 

François JOUANNE (Grenoble Univ., France) 

Anastasia KIRATZI (Aristotle Univ., Thessaloniki, Greece) 

Ibrahim MILUSHI (Institute of Geosciences, Tirana, Albania) 

Giuseppe NARDI (Univ. Federico II, Naples, Italy) 

Adil NEZIRAJ (Geological Survey, Tirana, Albania) 

Luan NIKOLLA (National Agency of Natural Resources, Tirana, Albania) 

Frederik PREMTI (PUTirana, Albania) 

Magdalena SCHECK-WENDEROTH (GFZ, Germany) 

Rudy SWENNEN (KU-Leuven) 

Bruno TOMJELOVIC (Zagreb Univ., Croatia) 

Fied Trips committee 

Çerçir DURMISHI (PUTirana, Albania) 

Avni MESHI (PUTirana, Albania) 

Bardhyl MUCEKU (PUTirana) 

Kujtim ONUZI (Institute of Geosciences, Tirana, Albania)

Nr. Prénom NOM Afilation 

1 Myqerem TAFAJ Minister of Education and Sciences 

2 Jorgaq KAÇANI Rector, Polytecnic University-Tirana 

3 Përparim HOXHA Dean, Faculty of Geology and Mines, PU-Tirana 

4 Arjan BEQIRAJ President, Albanian Geological Society 

Faculty of Geology and Mines, PU-Tirana 

5 Kristaq MUSKA Faculty of Geology and Mines, PU-Tirana 

6 Shaqir NAZAJ Faculty of Geology and Mines, PU-Tirana 

7 Çerçiz DURMISHI Faculty of Geology and Mines, PU-Tirana 

8 Andon GRAZHDANI Faculty of Geology and Mines, PU-Tirana 

9 Afat SERJANI Geological Survey of Albania 

10 Agim GUCAJ Geological Survey of Albania 

11 Ilia FILI Vizoka Energy, Albania 

12 Ajet MEZINI Vizoka Energy, Albania 

13 Alfred FRASHERI Faculty of Geology and Mines, PU-Tirana 

14 Gjergji FOTO Faculty of Geology and Mines, PU-Tirana 

15 Thoma KORINI Faculty of Geology and Mines, PU-Tirana 

16 Brunilda BRUSHULLI Faculty of Geology and Mines, PU-Tirana 

17 Luan NIKOLLA National Agency, Tirana 

18 Salvatore BUSHATI Academy of Sciences, Tirana 

19 Vilson SILO Faculty of Geology and Mines, PU-Tirana 

20 Erald SILO Faculty of Geology and Mines, PU-Tirana 

21 Irakli PRIFTI Faculty of Geology and Mines, PU-Tirana 

22 Bardhyl MUCEKU Faculty of Geology and Mines, PU-Tirana 

23 Ariana BEJLERI Polytechnic University-Tirana 

24 Flutura HAFIZI Polytechnic University-Tirana 

25 Shpresa SHUBLEKA Polytechnic University-Tirana 

26 Rrapo ORMENJI Polytechnic University-Tirana 

27 Viktor DODA Polytechnic University-Tirana 

28 Shkëlqim DAJA Faculty of Geology and Mines, PU-Tirana 

29 Jakup HOXHAJ Polytechnic University-Tirana 

30 Fatbardha CARA Polytechnic University-Tirana 

31 Hasan KULIÇI Polytechnic University-Tirana 

32 Sheribane ABAZI Polytechnic University-Tirana 

33 Rexhep KOÇI Polytechnic University-Tirana 

34 Neki KUKA Polytechnic University-Tirana 

35 Myslym PASHA Polytechnic University-Tirana 

36 Siasi KOCIU Polytechnic University-Tirana 

37 Artan TASHKO Faculty of Geology and Mines, PU-Tirana 

38 Ibrahim MILUSHI Polytechnic University-Tirana 

39 Gjon KAZA Polytecnic University-Tirana 

40 Avni MESHI Faculty of Geology and Mines, PU-Tirana 

41 Mensi PRELA Faculty of Geology and Mines, PU-Tirana 

42 Suada LUZATI Faculty of Geology and Mines, PU-Tirana 

43 Majlinda CENAMERI Faculty of Geology and Mines, PU-Tirana 

44 Flora PROGNI Faculty of Geology and Mines, PU-Tirana 

45 Neritan SHKODRANI Faculty of Geology and Mines, PU-Tirana 

46 Elsa DINDI Faculty of Geology and Mines, PU-Tirana

47 Vangjel MELO Faculty of Geology and Mines, PU-Tirana 

48 Ervin LULA Polytechnic University-Tirana 

49 Agim MESONJESI Polytechnic University-Tirana 

50 Edmond DUSHI Polytechnic University-Tirana 

51 Ylbert MUCEKU Polytechnic University-Tirana 

52 Jani SKRAMI Polytechnic University-Tirana 

53 Mehmet ZAÇAJ Polytechnic University-Tirana 

54 Piro LEKA Polytechnic University-Tirana 

55 Petrika KOSHO Polytechnic University-Tirana 

56 Petraq NAÇO Polytechnic University-Tirana 

57 Fatbardha VINÇANI Polytechnic University-Tirana 

58 Agim SINOJMERI Faculty of Geology and Mines, PU-Tirana 

59 Ana QORRI Faculty of Geology and Mines, PU-Tirana 

60 Eralda DAJA Faculty of Geology and Mines, PU-Tirana 

61 Erind ZAÇE Faculty of Geology and Mines, PU-Tirana 

62 Frederik PREMTI Polytechnic University-Tirana, 

Director of International Relations 

63 Kujtim ONUZI Polytecnic University-Tirana 

64 Adil NEZIRAJ Geological Survey, Tirana, Albania 

65 Zamir BEGA OMV, Buccarest, Romania 

66 Betim MUCO General Dynamics Inc., Rockville, USA 

67 Roland BARBULLUSHI Baropex, UK 

68 Skender LIPO Faculty of Geology and Mines, PU-Tirana 

69 Edmond HOXHA Faculty of Geology and Mines, PU-Tirana

6th workshop of the ILP Task Force on Sedimentary Basins 

Monday, November 8, 2010 

Tirana 

9- 10h30: Opening Session (chairs: Kristaq Muska and Magdalena Scheck-Wenderoth) 

9-9h15: Welcome addresses by: 

Pr. Dr. Myqerem Tafaj (Minister of Education and Sciences, Albania) 

Pr.Dr. Jorgaq Kaçani (Rector, PU-Tirana) 

Pr. Dr. Perparim Hoxha (Dean, Faculty of Geology and Mines, PU-Tirana) 

Pr.Dr. Arian Beqiraj (President , Albanian Geological Society) 

9h15-9h45: Sierd Cloetingh (ILP President, VU-Amsterdam): Aims and perspectives of 

ILP and Topo-Europe. 

9h45-10h15: Stefan Schmid, Daniel Bernoulli, B. Fügenshuh, Liviu Matenco, Roland 

Oberhänsli, S. Schlefer and K. Kustaszevski (univ. of Basel, VU- 

Amsterdam, Univ. of Potsdam): The Dinarides-Hellenides as a part of the 

Carpathians-Alps system: ancient and recent reorganization of a complex 

system of mountain chains. 

10h15-10h45: Hendrik Vogel, B. Wagner, T. Wilke, A. Grazhdani, G. Kostoski, S. 

Krastel, K. Reicherter and G. Zanchelta (univ. of Köln, Geomar, univ. of 

Aachen and Pisa): SCOPSCO: Scientific Collaboration on Past Speciation 

Conditions in Lake Ohrid (Albania/Macedonia): towards an ICDP deep 

drilling. 

10h45-11h10: Coffee Break and Poster Sessions 

11h10-12h30: Circum-Mediterranean, Alpine and Carpathians foreland-and-thrust belt 

systems and analogues (Part I) (chairs: Stefan Schmid and Shaqir Nazaj) 

11h10-11h30: Roland Barbullushi (Baropex, UK): Structural evolution of southern Albania 

thrust belt. 

11h30-11h50: Afat Serjani and Agim Gucaj (Geological Survey of Albania, Tirana): 

Correlation of the western structures of Ionian Zone and the relation with 

African plate (Adria micro-plate). 

11h50-12h10: Andrea Argnani (CNR, Bologna): Variations in structural style along the 

front of the Albanides fold belt and the heritage of Mesozoic palaeogeography. 

12h10-12h30: Piero Casero and François Roure (Rome and IFPEnergiesNouvelles): 

Geological meaning of the Sazani zone (Albania), implications on the regional 

paleogeographic setting. 

12h30-14h: Lunch Buffet 

14-15h30: Circum-Mediterranean, Alpine and Carpathians foreland-and-thrust belt 

systems and analogues (Part II) (chairs: Afat Serjani and Dirk Nieuwland) 

I

14-14h30: Liviu Matenco and M. Ducea (VU-Amsterdam and univ. of Arizona): On the 

link between orogenic shortening and "back-arc" extensional collapse in low 

topography orogens. 

14h30-14h50: Nico Hardebol and Giovanni Bertotti (univ. of Delft and VU-Amsterdam): 

Contraction and vertical movements in the Gargano Promontory and adjacent 

offshore: implication for the tectonics of the South Adriatic domain. 

14h50-15h10: François Roure, Piero Casero, and Belkacem Addoum 

(IFPEnergiesNouvelles, Rome and Sonatrach): Lateral and temporal evolution 

of the Alpine inversion of the North African margin from the Tellian Atlas to 

the Ionian Basin and Eastern Mediterranean. 


15h40-17h10: Back-arc and post-orogenic extension (chairs: Jean-Louis Mugnier and Liviu 

Matenco) 

15h40-16h: Alfonsa Milia, Eugenio Turco and Maurizio Torrente (CNR, Naples, univ. 

of Sannio): Four dimensional geological evolution of the Eastern Tyrrhenian 

Margin and geodynamic implications 

16h-16h20: Mary Ford (univ. of Nancy, CRPG): Corinth rifting and its role in the 

geodynamic evolution of the Aegean-Ionian region. 

16h20-16h40: Nadine Ellouz-Zimmermann, Raymi Castilla and François Roure 

(IFPEnergiesNouvelles): Impact of basement configuration and sediment 

architecture on gravity gliding on under-compacted shale decollements. 

16h40-17h: Christophe Pascal, Aline Saintot, A. Nasuti, E. Lunberg and C. Juhlin 

(NGU, Norway, and univ. of Uppsala, Sweden): An integrated study of the 

MØre-TrØndelag fault complex, Mid Norway. 

17h-18h30: Poster Sessions 

Tuesday, November 9, 2010 

9-12h30: Albanian exploration, petroleum systems and analogues (Part I) (Chairs: 

Ilia Fili and Ibrahim Milushi) 

9-9h30: Zamir Bega (OMV-Petrom): Platform carbonate subthrusts as major 

hydrocarbon plays in NW Albania-Montenegro region. 

9h30-9h50: Alfred Frasheri (Polytechnic univ., Tirana): Geophysical outlook on structure 

of the Albanides. 

9h50-10h20: Dirck Nieuwland (NewTec International BV, Leiden): The mechanics of 

thrust tectonics, the evolution of the Albanides and implications for 

hydrocarbon exploration. 


10h50-11h10: Anne Jardin, Luan Nikolla and François Roure (IFPEnergiesNouvelles and 

National Agency, Tirana): Subsalt depth seismic imagery and structural 

interpretation in the Dumre area, Albania. 

II

11h10-11h30: Vilson Silo, Salvatore Bushati and Erald Silo (Polytechnic univ., Tirana): 

Gas detection in the Peri-Afriatic Depression area by true amplitude processing 

of seismic data. 

11h30-11h50: Irakli Prifti and Kristaq Muska (Polytechnic univ., Tirana): Hydrocarbon 

occurrences and petroleum geochemistry of Albanian oils. 

11h50-12h10: Alfred Frasheri (Polytechnic univ., Tirana): Temperature signals from 

Albanides depth. 

12h10-13h40: Lunch Buffet 

13h40-16h40: Albanian exploration, petroleum systems and analogues (Part II) (Chairs: 

Salvatore Bushati and Zamir Bega) 

13h40-14h10: Ruddy Swennen (KU-Leuven): Diagenetic history of Cretaceous carbonate 

reservoir analogues of the Ionian and Kruja zones. 

14h10-14h30: Çerçis Durmishi (Polytechnic univ., Tirana): Sequence statigraphy of deepwater 

Serravalian siliciclastics of the Zverneci outcrop (Vlora region, Albania). 

14h30-14h50: Vilson Silo, Kristaq Muska and Erald Silo (Polytechnic univ., Tirana): 

Hydrocarbon potential in Molasse reservoirs, Vlora-Elbasan region, Albania. 

14h50-15h10: Brunilda Brushulli and Gjergji Foto (Polytechnic univ., Tirana): Use of 

capillary pressure measurements to assess the flow units in oil-bearing 

carbonate reservoirs of the Albanian Ionian Zone. 


15h40-16h: Yvonne Cherubini, Mauro Cacace, Magdalena Scheck-Wenderoth, 

Mando Guido Blöcher and Björn Lewerenz (GFZ): Impact of single faults 

on the fluid flow and heat transport: first results from 3D finite elements 

simulations. 

16-16h20: François Roure, Laurie Barrier, Jean-Paul Callot, Kristaq Muska and 

Nadège Vilasi (IFPEnergiesNouvelles, Polytechnic univ., Tirana): Kinematic 

and petroleum modelling in the Albanides. 

16h20-16h40: Magdalena Scheck-Wenderoth (GFZ): Shallow and deep control on the 

thermal structure of basins as inferred by 3 D numerical models: examples 

from the Central European Basin System. 

16h40-17h40: Mantle tomography, lithospheric and crustal architecture (chairs: Sierd 

Cloetingh and Betim Muco) 

16h40-17h: Abdullah Al Amri (King Saud Univ., Riyad): Seismic sources zones of the 

Arabian Peninsula and adjacent countries. 

17h-17h20: Abdullah Al Amri and Arthur Rodgers (King Saud Univ., Riyad): Structure 

of the lithosphere and upper mantle across the Arabian Peninsula. 

17h20-17h40: Magdala Tesauro, Mikhail Kaban and Sierd Cloetingh (GFZ and VU- 

Amsterdam): Strengh and weakness of the World lithosphere. 

Wednesday, November 10, 2010 

8h20-13h10: TOPO-Albania (chairs: Bardhyl Muceku and Hendrik Vogel) 

III

8h20-8h50: Anastasia Kiratzi (Aristotle univ. of Thessaloniki): Seismic sequences in 

Dibra region (Albania) and implications for the seismic hazard of the region. 

8h50-9h10: Ariana Bejleri, Flutura Hafizi and Shpresa Shubleka (Polytechnic univ., 

Tirana): Analyzing seismic situation in the Dibra region by digitalization of 

seismic events. 

9h10-9h40: Betim Muco (General Dynamics Inc., USA): ALBASEIS, risk assessment and 

seismicity of Albania.: 

9h40-10h: Rrapo Ormeni, Shkelqim Daja and Viktor Doda (Polytechnic univ., 

Tirana): The strongest earthquakes occurred in Albania during 2009 (M>5.0) 

and their seismogenic zones. 

10h-10h20: Olivier Lacombe, Nadège Vilasi and François Roure (univ. Paris VI and 

IFPEnergiesNouvelles): From paleostress to paleoburial in fold-thrust belts: 

Preliminary results from calcite twin analysis. 


10h40-11h10: Christian Beck (univ. of Savoie, Chambéry): Sedimentological contribution to 

seismic hazards assessment: Lacustrine and marine archives along active fault 

systems. 

11h10-11h30: Jakup Hoxhaj, Fatbardha Cara, Hasan Kuliçi and Sheribane Abazi 

(Polytechnic univ., Tirana, and Geological Survey of Albania): Stratigraphy 

and lithological composition of the Quaternary sedimentation in the Albanides. 

11h30-12h: François Jouanne, Jean-Louis Mugnier, Rexhep Koçi, S. Bushati, K. 

Matev, N. Kuka, I. Shiviko, M. Pasha. and S. Kociu (univ. of Savoie, 

Chambéry, and Institute of Seismology, Tirana): GPS constrains on current 

tectonics of Albania. 

12h-12h20: Bardhyl Muceku, Georges H. Mascle, Peter van der Beek, Matthias 

Bernet, Peter Reiners and Artan Tashko (PT University, Tirana, univ. 

Grenoble): Low temperature thermochronometry in Internal Albanides: 

Quantitative constraints on exhumation rate and tectonic implications. 

12h20-12h40: Klaus Reicherter, Katja Lindhorst, Nadine Hoffmann, Sebastian Krastel- 

Gudegast, Ariane Liermann and Ulrich Glasmacher (univ. of Aachen and 

Heidelberg, and Geomar, Kiel): Active basins and neotectonics: 

morphotectonics of the Lake Ohrid Basin (FYROM and Albania). 

12h40-13h: Oswaldo Guzman, Jean-Louis Mugnier, Rexhep Koçi, R. Vassallo, Julien 

Carcaillet and E. Fouache (univ. of Savoie, Chambéry, and Institute of 

Seismology, Tirana): Active tectonics of Southern Albania inferred from Pre- 

LGM fluvial terraces geometries. 

13-14h: Lunch Buffet 

14-14h20: Shkëlqim Daja and Neritan Shkodrani (Polytechnic University, Tirana): A 

case study on probalistic evaluation of soil liquefaction. 

14h20-15h40: Albanian volcanics and ophiolites (chairs: Olivier Lacombe and Angela 

Jayko) 

1420-14h40: Ibrahim Milushi, Avni Meshi and Gjon Kaza (Polytechnic univ., Tirana): 

Volcano-sedimentary formations in Albania and their relation with the Mirdita 

Ophiolite. 

IV

14h40-15h: Ariana Bejleri, Mensi Prela and Flutura Hafizi (Polytechnic univ., Tirana): 

Digitalization of data related to the age of Albanian Ophiolites. 

15h-15h20: Mensi Prela (Polytechnic univ., Tirana): Stratigraphic correlation of 

radiolarian cherts belonging to the ophiolite-bearing and carbonatic 

successions 

15h20-15h40: Artan Tashko and Georges Mascle: (Polytechnic univ., Tirana, and univ. of 

Grenoble) Geochemical constraints (Nd, Pb isotopse ratios and trace elements) 

on the Mesozoic volcanism in Albania. 

15h40-16h20: Pannel discussion on the Albanian natural laboratory and conclusions. 

(Chairs: François Roure, Kristaq Muska, Liviu Matenco and François Jouanne) 

17h30: Departure for the post-conference fieldtrip 

List of Posters 

Laurie Barrier, Emily Albouy, Sazan Guri, Jean-Luc Rudkiewicz, Spiro Bonjakes, 

Kristaq Muska and Rémi Eschard (IPGP and IFPEnergiesNouvelles): Structural and 

stratigraphic history of the Outer Albanides from restored cross-sections, 

chronostratigraphic chart and coupled kinematic/stratigraphic forward modelling. 

Arjan Beqiraj, Suada Luzati and Majlinda Cenameri (Polytechnic University, Tirana): 

Hydrochemical features of the Kavaja groundwater basin (Preadriatic Depression, 

Albania). 

Arjan Beqiraj, F. Progni and Majlinda Cenameri (Polytechnic University, Tirana): 

Groundwater vulnerability assessment to contamination (Tirana-Fiske Kupe Basin, 

Albania). 

Elsa Dindi (Polytechnic University, Tirana): The role of geological factor in the chemical 

content of the Quaternary gravel aquifers of the Preadriatic Depression. 

Cerçis Durmishi and Shkelqim Daja (Polytechnic University, Tirana): Spectacular evidence 

of sedimentary structures of the Serravalian deposits in the Zverneci outcrops (Albania). 

Cerçis Durmishi, Vangjel Melo and Ervin Lula (Polytechnic University, Tirana): Kink 

bands and chevron folds characteristics of the Saranda Anticline: Estimation of the 

Geologist's mosaic, southwestern Albania. 

Edmond Dushi, Ylbert Muceku, J. Skrami and M. Zaçaj (Polytechnic University, Tirana): 

Instrumental seismological data and geophysical investigation of 2009 earthquake at 

Gjorica, Dibra Region, Albania). 

Gjergji Foto, Ilia Fili, Thoma Korini and Brunilda Brushulli (Polytechnic univ., Tirana): 

Tectonic movements in the Kremenare-Ballsh structures can hide new oil and gas traps. 

Rexhep Koçi, Agim Mesonjesi, Jean-Louis Mugnier, François Jouanne, Julien Carcaillet 

and Oswaldo Guzman (Institute of Geosciences, Tirana, and univ. of Savoie, 

Chambéry): River Terraces and their age determination in Albania. 

Piro Leka, Petrika Kosho, Petraq Naço and Fatbardha Vinçani (Institute of Geosciences, 

Tirana): Identification of the neotectonic movements through geophysical methods in 

the Elbasan basin 

Ajet Mezini and Ilia Fili (Vizoka Energy):Hydrodynamic conditions of the Visoka field 

trapping. 

Maghfouri Moghddam (univ. of Lorestan, Iran): Biostratigraphy of the Tarbur Formatrion, 

Zagros Basin. 

V

Ylbert Muceku, Jani Skrami, Edmond Dushi and Mehmet Zaçaj (Polytechnic University, 

Tirana): The engineering geological and geophysical studies of land-use planning in 

Adriatic Coastal Plains-Divjaka, Albania. 

Kristaq Muska (Polytechnic University, Tirana): Thermal evolution, hydrocarbon generation 

and HC potential of Triassic and Liassic carbonate reservoirs in the Ionian Zone 

(Albania). 

Rrapo Ormeni and Shaqir Nazaj (Polytechnic univ., Tirana): 1D-velocity models and 

lateral contrasts in zones divided from Shkoder-Peja fault of Albania. 

Mensi Prela (Polytechnic univ., Tirana): The age of radiolarian cherts in the western 

carbonate peripheral units of the Albanian ophiolites. 

Yolaine Rubert, Mohamed Jati, Corinne Loisy, Adrian Cerepi, Gjergji Foto and Kristaq 

Muska (Bordeaux Univ., France, Polytechnic Univ., Tirana): Sedimentology of 

resedimented carbonates: facies and geometrical characterization of Upper Cretaceous 

calciturbidite system in Albania. 

Yolaine Rubert, Mohamed Jati, Corinne Loisy, Adrian Cerepi, Gjergji Foto and Kristaq 

Muska (Bordeaux Univ., France, Polytechnic Univ., Tirana): Reservoir properties of 

resedimented carbonates: petrophysical characterization of Upper Cretaceous turbiditic 

systems in Albania. 

Agim Sinojmeri, Cerçis Durmishi, Ana Qorri, Eralda Daja and Erind Zaçe (Polytechnic 

University, Tirana): Recent sediments on Vjosa River deltaic littoral. 

Nadège Vilasi, Jean-Paul Callot, Kristaq Muska, François Roure and Ruddy Swennen 

(IFPEnergiesNouvelles, Polytechnic univ., Tirana, and KU-Leuven: Characterization of 

the fluid flow in the Albanides foreland fold-and-thrust belts (Southern Albania). 

VI

ABAZI Sheribane 71 

ADDOUM Belkacem 155 

AL AMRI Abdullah 1 

ALBOUY Emily 11 

Al HOSANI Khalid 55 

Al MAHMOUDI Saleh 55 

ARGNANI Andrea 5 

BARBULLUSHI R. 9 

BARE Vilson 61 

BARRIER Laurie 11, 149 

BECK Christian 

BEGA Zamir 13 

BEJLERI Ariana 17, 19 

BEQIRAJ Arjan 21, 27 

BERNET Matthias 111 

BERNOULLI Daniel 167 

BERTOTTI Giovanni 67 

BLOCHER Mando Guido 35 

BONJAKES Spiro 11 

BRUSHULLI Brunilda 31 

BUSHATI Salvatore 61, 75, 181 

CACACE Mauro 35, 165 

CALLOT Jean-Paul 149, 197 

CARA Fatbardha 71 

CARCAILLET Julien 63, 81 

CASERO Piero 155 

CASTILLA Raymi 51 

CENAMERI Majlinda 21, 27 

CEREPI Adrian 157, 161 

CHERUBINI Yvonne 35 

CLOETINGH Sierd 37, 193 

DAJA Eralda 183 

DAJA Shkelqim 39, 45, 125 

DINDI Elsa 41 

DODA Viktor 129 

DUCEA M. 95 

DURMISHI Cerçis 43, 45, 47, 183 

DUSHI Edmond 51, 109 

ELLOUZ-ZIMMERMANN Nadine 55 

ESCHARD Rémi 11 

FILI Ilia 97 

FOTO Gjergji 31, 157, 161 

FOUACHE E. 63 

FRASHERI Alfred 59, 61 

FORD Mary 57 

FUGENSHUH B. 167 

GAHNOOG Abdullah 55 

GLASMACHER Ulrich 149 

CONTENTS 

VII 

GRAZHDANI A. 199 

GUCAJ Agim 173 

GURI Sazan 11 

GUZMAN Oswaldo 63, 81 

HAFIZI Flutura 17, 19 

HARDEBOL Nico 67 

HOFFMANN Nadine 149 

HOXHAJ Jakup 71 

JARDIN Anne 73 

JATI Mohamed 157, 161 

JOUANNE François 63, 75, 81 

JUHLIN C. 133 

KABAN Mikhail 193 

KAZA Gjon 105 

KIRATZI Anastasia 77 

KOCI Rexhep 63, 75, 81 

KOCIU S. 75 

KORINI Thoma 

KOSHO Petrika 89 

KOSTOSKI G. 199 

KRASTEL S. 199 

KRASTEL-GUDEGAST Sebastian 149 

KUKA N. 75 

KULICI Hasan 71 

KUSTASZEVSKI K 

LACOMBE Olivier 87 

LEKA Piro 89 

LEWERENZ Björn. 35 

LIERMANN Ariane 149 

LINDHORST Katja 149 

LIPO Skender 93 

LOISY Corinne 157, 161 

LULA Ervin 47 

LUNBERG E. 129 

LUZATI Suada 21 

MASCLE Georges 11, 187 

MATENCO Liviu 95, 167 

MATEV K. 75 

MAYSTENKO Yuriy 165 

MELO Vangjel 47 

MESHI Avni 105 

MESONJESI Agim 81 

MEZINI Ajet 97 

MILIA Alfonsa 101 

MILUSHI Ibrahim 105 

MOGHDDAM Maghfouri 107 

MUCEKU Bardhyl 111 

MUCEKU Ylber 41, 109

MUCO Betim 113 

MUGNIER Jean-Louis 63, 75, 81 

MUSKA Kristaq 11, 117, 137, 149, 

157, 161, 179 

NACO Petraq 89 

NASUTI A. 129 

NAZAJ Shaqir 127 

NIEUWLAND Dirck 121 

NIKOLLA Luan 73 

OBERHANSLI Roland 167 

ORMENI Rrapo 125, 127 

PASCAL Christophe 129 

PASHA M. 75 

PRELA Mensi 17, 133, 136 

PRIFTI Irakli 137 

PROGNI F. 27 

QORI Ana 145, 183 

REICHERTER Klaus 149, 199 

REINERS Peter 111 

RODGERS Arthur 1 

ROURE François 55, 73, 87, 149, 155, 

197 

RUBERT Yolaine 157, 161 

RUDKIEWICZ Jean-Luc 11 

SAINTOT Aline 133 

SCHECK-WENDEROTH M. 35, 165 

SCHLEFER S. 167 

VIII 

SCHMID Stephan 167 

SERJANI Afat 173 

SHIVIKO I. 75 

SHKODRANI Neritan 39 

SHUBLEKA Shpresa 19 

SILO Erald 179, 181 

SILO Vilson 179, 181 

SINOJMERI Agim 183 

SKRAMI Jani 109 

SWENNEN Rudy 185, 197 

TASHKO Artan 111, 187 

TESAURO Magdala 193 

TORRENTE Maurizio 101 

TURCO Eugenio 101 

USTASZEWSKI K. 167 

van der BEEK Peter 111 

VASSALLO R. 

VILASI Nadège 87, 149, 197 

VINCANI Fatbardha 89 

VOGEL Hendrik 199 

WAGNER B. 199 

WILKE T. 199 

ZACAJ Mehmet 51, 109 

ZACE Erind 183 

ZANCHETTA G. 199

ILP TASK FORCE on SEDIMENTARY BASINS 

2010 International Workshop 

November 7-12, 2010, Tirana (Albania) 

STRUCTURE of the LITHOSPHERE and UPPER MANTLE 

across the ARABIAN PENINSULA 

Abdullah AL-AMRI 1 and Arthur RODGERS 2 

1. Seismic Studies Center and Geology Department, King Saud University Riyadh, SAUDI 

ARABIA, amri444@yahoo.com 

2. Seismology Group, Energy and Environment Directorate, Lawrence Livermore National 

Laboratory, Livermore CA USA, rodgers7@llnl.edu.org 

Analysis of the Arabian Peninsula presents several interesting seismological problems. On 

the west, rifling in the Red Sea has split a large Precambrian Shield. Active rifling is 

responsible for the geometry of the plate margins in the west, and southwest. To the south, 

similar rifling running in a more east-west direction through the Gulf of Aden has separated 

the Arabian Peninsula from Africa. In the northwest, the Gulf of Aqabah forms the 

southernmost continuation of the Dead Sea transform. The northern and northeastern 

boundaries of the Arabian Plate are areas of continental collision, with the Arabian Plate 

colliding with the Persian Plate (Fig. 1). 

Modern broadband (BB) waveform data allows for the inference of seismic velocity structure 

of the crust and upper mantle using a variety of techniques. This presentation will report 

inferences of seismic structure of the Arabian Plate using BB data from various networks. 

Most data were recorded by the Saudi Arabian National Digital Seismic Network (SANDSN) 

which consists of 38 (26 BB, 11 SP) stations, mostly located on the Arabian Shield. 

Additional data were taken from the 1995-7 Saudi Arabian IRIS-PASSCAL Deployment (9 

BB stations) and other stations across the Peninsula. 

Crustal structure, inferred from teleseismic P-wave receiver functions, reveals thicker crust 

in the Arabian Platform (40-45 km) and the interior of the Arabian Shield (35-40 km) and 

thinner crust along the Red Sea coast. Lithospheric thickness inferred from teleseismic Swave 

receiver functions reveals very thin lithosphere (60-80 km) along the Red Sea coast 

which thickens rapidly toward the interior of the Arabian Shield (100-120 km). We also 

observe a step of 20-40 km in lithospheric thickness across the Shield-Platform boundary. 

Seismic velocity structure of the upper mantle inferred from teleseismic P- and S-wave travel 

time tomography reveals large differences between the Shield and Platform, with the Shield 

being underlain by slower velocities, ±3% for P-waves and ±6% for S-waves. Seismic 

anisotropy was inferred from shear-wave splitting, using teleseismic SKS waveforms. 

1

Figure 1: Map of the Arabian Peninsula. Major tectonic features are indicated. Plate 

boundaries are indicated by yellow lines. Earthquakes and volcanic centers; shown as red 

circles and yellow diamond, respectively. 

Results reveal a splitting time of approximately 1.4 seconds, with the fast axis slightly east of 

north. The shear-wave splitting results are consistent across the Peninsula, with a slight 

clockwise rotation parallel for stations near the Gulf of Aqabah. In summary, these results 

allow us to make several conclusions about the tectonic evolution and current state of the 

Arabian Plate. Lithospheric thickness implies that thinning near the Red Sea has 

accompanied the rupturing of the Arabian-Nubian continental lithosphere. The step in the 

lithospheric thickness across the Shield-Platform boundary likely reveals a pre-existing 

difference in the lithospheric structure prior to accretion of the terranes composing the eastern 

Arabian Shield. Tomographic imaging of upper mantle velocities implies a single large-scale 

thermal anomaly underlies the Arabian Shield and is associated with Cenozoic uplift and 

volcanism. 

The Moho and LAB are shallowest near the Red Sea and become deeper towards the Arabian 

interior. Near the coast, the Moho is at a depth of about 22-25 km. Crustal thickening 

continues until an average Moho depth of about 35-40 km is reach beneath the interior 

Arabian Shield. The LAB near the coast is at a depth of about 55 km; however it also deepens 

beneath the Shield to attain a maximum depth of 100-110 km. These boundary depths are 

comparable to those at similar distances along profile AA’. At the Shield-Platform boundary, 

a step is observed in the lithospheric thickness where the LAB depth increases to about 160 

km. (Fig.2) 

2

Topography, sediment and 

basement 

Observed (dots) and 

predicted (line) gravity 

anomaly 

Lithospheric cross-section 

with shear velocities and 

densities 

basement 

sediment 

Figure 2: Topography, gravity signature, and lithospheric structure along the Arabian 

Peninsula. a Topography along the profile plotted with a 32x vertical exaggeration (V.E.). 

The sediment thickness is shown by the grey shaded areas. b Comparison of the observed 

gravity data from the GRACE satellites (black dots) and the calculated gravity (grey line) 

resulting from the structural model shown in c. The S-wave velocities (Vs) in km/s and 

densities (�) in g/cm3 of each layer are listed (Hansen et al.,2008). 

References 

Al-Amri, A. M. (1999). The crustal and upper mantle structure of the Interior Arabian 

Platform. Geophysical J. International, V. 136, pp. 421 - 430. 

Hansen, S., Gaherty, J., Schwartz, S., Rodgers, A., and Al-Amri, A. (2008). Seismic Velocity 

Structure and Depth-dependence of Anisotropy in the Red Sea and Arabian Shield 

from Surface Wave Analysis. Journal of Geophysical Research, Vol., 113 Doi : 

10.1029/2007JB005335. 

Park Y., Nyblade, A., Rodgers, A., and Al-Amri, A. (2007). Upper mantle structure beneath 

the Arabian Peninsula and Northern Red Sea from teleseismic body wave tomography: 

Implications for the origin of Cenozoic uplift and volcanism in the Arabian Shield. 

Geochem. Geophy. Geosys., 8, doi : 10.1029 / 2006 GC 001566. 

3




VARIATIONS in STRUCTURAL STYLE along the FRONT of the ALBANIDES 

FOLD BELT and the HERITAGE of MESOZOIC PALEOGEOGRAPHY 

Andrea ARGNANI 

ISMAR-CNR, Bologna, andrea.argnani@ismar.cnr.it 

Along strike variations in structural style occur at all scales, from outcrops to Fold-and-Thrust 

Belts (FTBs), as shape and size of thrust faults are controlled by strength heterogeneity and 

anisotropy of the rock units (Price, 1988). 

Frontal accretion is a critical step in the building of FTBs and often occurs in close 

relationship with sedimentation. In fact, the foredeep basins that are typically located at the 

front of FTBs (DeCelles and Giles, 1996) represent a very dynamic setting where tectonics 

and sedimentation interact closely, giving rise to a variety of growth strata geometries (Suppe 

et al., 1992). Furthermore, sedimentary load combines with thrust load to localize the 

successive thrust faults as both contribute to stabilize the footwall (Goff and Wiltschko, 

1992), ultimately controlling the spacing of thrust sheets. 

Topography of the foreland is likely to play a role in controlling the frontal accretion of FTBs. 

Although this aspect has never been addressed specifically, positive features impinging the 

accretionary wedge in oceanic subduction settings have been shown to greatly affect both 

thrust geometry and wedge topography (Lallemand and Le Pichon, 1987; McCann and 

Habermann, 1989; Dominguez et al., 2000). 

This contribution addresses some geological factors controlling the large-scale variations in 

structural style of FTBs, as observed at the Albanide thrust front. The structure and evolution 

of the Albanide fold-and-thrust belt has been well worked out thanks to good quality outcrops 

and subsurface exploration (Papa, 1970; Velaj, et al.,1999; Niewland et aal., 2001; Roure et 

al., 2004). However, only limited information are available in the public domain for the 

Albanina offshore (Ballauri et al., 2002) and palaeogeographic reconstructions lack reliable 

constraints (e.g., Robertson and Shallo, 2000). The front of the W-verging Albanide foldand-thrust 

belt and its adjacent foreland have been investigated using a grid of seismic 

reflection profiles, purposely acquired in the Southern Adriatic Sea (Argnani et al., 1994, 

1996). 

The analysisi of seismic profiles shows that the structural style of the external part of the foldand-thrust 

belt and the evolution of the related foredeep basin (Fig. 1) are strongly controlled 

by the nature of the Mesozoic units that are progressively accreted to the belt, namely the 

Apulian Platform and its adjacent deep-water basins: The impingement of the FTB on 

platform-to-basin Mesozoic domains, trending at an angle with respect to the thrust front, can 

account for the observed large-scale variation in structural style. Moreover, the structural 

contour map of the base of the Oligo-Miocene clastic succession (Fig. 1) indicates that also 

the foredeep development is largely controlled by the Mesozoic paleogeography, with larger 

thickness reached offshore of northern Albania where the Mesozoic pelagic basin is located 

(Fig. 2). Finally, the along strike variation in mechanical stratigraphy at the thrust front is 

promoting the growth of an incipient basin-controlled salient (Macedo and Marshak, 1999) 

north of the thick Apulian platform carbonates (Fig. 1), where the foredeep sedimentary fill 

reaches its maximum thickness. 

5

REFERENCES 

Argnani A., Favali P., Frugoni F., Gasperini M., Ligi M., Marani M., Mattietti G. and Mele 

G., 1993, Foreland deformational pattern in the Southern Adriatic Sea. Ann. Geof., 36, 

229-247. 

Argnani A., Bortoluzzi G., Favali P., Frugoni F., Gasperini M., Ligi M., Marani M., Mattietti 

G. and Mele G., 1994, Foreland Tectonics in the Southern Adriatic Sea. Mem. Soc. Geol. 

It., 48, 573-578. 

Argnani A., Bonazzi C., Evangelisti D., Favali P., Frugoni F., Gasperini M., Ligi M., Marani 

M. and Mele G., 1996, Tettonica dell'Adriatico meridionale. Mem. Soc. Geol. It., 51, 227- 

237. 

Ballauri A., Bega Z., Meehan P., Gambini R. and Klammer W., 2002, Exploring in 

structurally complex thrust belt: Southwest Albania Case. AAPG Hedberg Conference, 

May 14-18, 2002, Palermo-Mondello (Sicily, Italy). 

DeCelles P.G. and Giles K.A., 1996, Foreland basin systems. Basin Research 8, 105-123. 

Dominguez S., Malavieille J. and Lallemand S.E., 2000, Deformation of accretionary wedges 

in response to seamount subduction: insights from sandbox experiments. Tectonics, 19, 

182-196. 

Goff D. and Wiltschko D.W., 1992, Stresses beneath a ramping thrust sheet. J. Struct. Geol., 

14, 437-449. 

Lallemand S. and Le Pichon X., 1987, Coulomb wedge model applied to the subduction of 

seamounts in the Japan Trench. Geology, 15, 1065-1069. 

Macedo J. and Marshak S. (1999) Controls on the geometry of fold-thrust belt salients. Geol. 

Soc. Am. Bull., 111, 1808-1822. 

McCann W.R. and Habermann R.E., 1989, Morphologic and geologic effects of the 

subduction of bathymetric highs. PAGeoph., 129, 41-69. 

Nieuwland D.A., Oudmayer B.C. and Valbona U., 2001, The tectonic development of 

Albania: explanation and prediction of structural styles. Marine and Petrol. Geol., 18, 161- 

177. 

Papa A., 1970, Conceptions nouvelles sur la structure des Albanides (presentation de la Carte 

tectonique de l’Albanie au 1/500 000). Bull. Soc. geol. de France, 12, 1096-1109. 

Price R.A., 1988, The mechanical paradox of large overthrusts. Geol. Soc. Am. Bull., 100, 

1898-1908. 

Robertson A. and Shallo M., 2000, Mesozoic-Tertiary tectonic evolution of Albania in its 

regional Eastern Mediterranean context. Tectonophys., 316, 197-254. 

Roure F., Nazaj S., Mushka K., Fili I., Cadet J.-P. and Bonneau M., 2004, Kinematic 

evolution and petroleum systems - an appraisal of the Outer Albanides. In: K.R. McClay, 

Thrust tectonics and hydrocarbon systems. AAPG Mem., 82, 474-493. 

Suppe J., Chou G.T. and Hook S.C., 1992, Rates of folding and faulting determined from 

growth strata. In: Thrust Tectonics, K.R. McClay (ed), Chapman and Hall, 105-121. 

Velaj T., Davison I., Serjani A. and Alsop I., 1999, Thrust tectonics and the role of evaporites 

in the Ionian Zone of the Albanides. AAPG Bull., 83, 1408-1425. 

6

Fig. 1: Isochron map (seconds, TWT) of base of the Southern Adriatic foredeep clastic 

succession. The foredeep basin is deeper on top of the Mesozoic pelagic basin (white; 

horizontal rules in outcrop) and becomes markedly shallower over the Mesozoic carbonate 

platform (brick pattern; outcrop shaded). The margin of the Mesozoic carbonate platform 

(ticked line) and the principal Neogene structures identified in the Southern Adriatic are 

shown. Note that the NNW-SSE folds in the centre of the southern Adriatic Sea affect only 

the clastic fill of the foredeep basin. The roughly E-W trending structures in the top left are 

due to foreland tectonics (Argnani et al., 1993). D Dumre diapir; V-E Vlore-Elbassan 

transversal line. 

Fig. 2: Profile ADS 02 crossing the northern and deepest portion of the Southern Adriatic 

foredeep basin. The reflector marking the base of the clastic foredeep sequence dips eastward 

down to 8 seconds (TWT). The upper part of the foredeep sedimentary fill is involved, near 

the Albanian coast, in a large scale backthrust. 

7




STRUCTURAL EVOLUTION of SOUTHERN ALBANIA THRUST BELT 

Dr Roland BARBULLUSHI 

Baropex Ltd. roland@baropex.co.uk 

The southern Albania thrust belt comprises Mesozoic-Eocene carbonate sequences 

incorporated into three major Tertiary thrust sheets verging towards the Apulia foreland in the 

southwest. The problem of the structural evolution has been previously approached through a 

hypothesis of orthogonal thin-skinned thrusting controlled by a differential areal extent of 

Permo-Triassic evaporites. 

This research uses the interpretation of several seismic profiles to address questions such as 

those relating to the subsurface geometric patterns of the thrust sheets, the kinematic 

framework the evaporites operated in, the role of the pre-existing faults and the timing of the 

evolution. 

The interpretation demonstrates that significant along-strike changes characterize the 

subsurface geometry of the thrust sheets. The Permo-Triassic evaporites facilitated their 

buttressing against a buffer zone in the Apulian foreland primarily within an orthogonal 

compressional regime. Regional clockwise rotation about a pivot point to the north may have 

provided a transpressional component along the thrusts. Pre-existing normal faults played a 

significant role in thrusting and accommodation of the strain partitioning. The main structural 

events included thin-skinned thrusting during Oligocene-Aquitanian, formation of a buffer 

zone in the foreland during the Burdigalian and subsequent thrust - buttressing during the 

Miocene. Post-Pliocene deformation occurs in the foredeep basin. 

9




STRUCTURAL and STRATIGRAPHICAL HISTORY of the OUTER ALBANIDES 

from 

RESTORED STRUCTURAL CROSS-SECTIONS, 

CHRONOSTRATIGRAPHIC CHART 

and 

COUPLED KINEMATIC/STRATIGRAPHIC FORWARD MODELLING 

Laurie BARRIER 1 , Emily ALBOUY 2 , Sazan GURI 3 , Jean-Luc RUDKIEWICZ 2 , Spiro 

BONJAKES 3 , Kristaq MUSKA 3 and Rémi ESCHARD 2 

(1) Équipe de Tectonique et Mécanique de la Lithosphère, Institut de Physique du Globe de 

Paris (Institut associé au CNRS et à l’Université de Paris 7), 1 rue Jussieu, 75238 Paris 

Cedex 05, France 

Tel: +33.(0)1.83.95.76.08, Email: barrier@ipgp.fr 

(2) Département de Géologie-Géochimie, IFP Energies Nouvelles, 1 & 4 Avenue de Bois- 

Préau, 92852 Rueil-Malmaison Cedex, France 

(3) Polytechnic University, Tirana, Albania 

In orogenic systems, the relationships between deformation and sedimentation are essential 

keys to understand the structure and evolution of fold and thrust belts and foreland basins. 

Joint structural and stratigraphic studies can therefore provide very interesting results. In this 

perspective, we used such a joint approach to bring new constraints on the structural, 

erosional and depositional events that occurred in the Outer Albanides during the Cenozoic. 

In their central part, the Outer Albanides show a typical fold-and-thrust belt where the syncompression 

sediments are very well preserved. First, two regional seismic sections were 

interpreted, balanced and unfolded to provide a structural picture of the study zone at different 

times during compression. A synthetic chronostratigraphic chart of Albanian syn-tectonic 

deposits was also drawn from field, well and seismic data. Based on the previous geological 

model, a coupled structural and stratigraphic forward modelling of the Outer Albanides was 

finally carried out using the Thrustpack and Dionisos softwares (© IFP). 

This coupled modelling allowed us to iteratively correct and refine the structural and 

stratigraphic geometry and history of the study area interpreted from the surface and 

subsurface data. The modelling also leads us to quantify the sedimentary transfers in this 

region in response to the thin- and thick-skin deformation into the fold-and-thrust belt. 

11




PLATFORM CARBONATE SUBTHRUSTS as MAJOR HYDROCARBON PLAYS in 

NW ALBANIA - MONTENEGRO REGION 

Zamir BEGA, 

OMV PETROM S.A., Romania 

e-mail: zamir.bega2@petrom.com 

Until to date, most of the industry exploration efforts in the NW Albania-Montenegro region 

(Fig. 1) have been focused either towards the thin-skinned thrust of Kruja-Dalmatian platform 

carbonate ramps or outboard of Kruja-Dalmatian thrust front, searching for pelagic thrusted 

ramps. Both approaches resulted unsuccessful despite abundant hydrocarbon shows in the 

area. All deep wells drilled outboard of Kruja thrust front have TD at Tertiary deposits, failing 

to reach the Mesozoic target. 

The new data gathered by international industry during 90’s provides new insights to the 

Mesozoic paleogeography and Mesozoic platform/basin morphology. Two major tectonic 

units, which differ only in deformation style can be deciphered in onshore-offshore Albania- 

Montenegro: the thick-skin deep seated platform to the west, partly inverted, as part of 

Apulian foreland eastward ramp, and a wide zone to the east, characterized by the known 

Kruja-Dalmatian thin-skinned ramps, running parallel to the coast line. JJ-3 well (offshore 

Montenegro) is the only well that have been reached the thick skinned platform carbonates. 

Delineation of the thick-skin platform margin towards the offshore-onshore Albania was 

carried out based on new 2D seismic lines acquired during 90’s (Fig. 2). 

The relationships between the thick-skinned platform carbonates and the thin-skinned ones 

are product of pre-orogeny architecture and also foreland-ward contraction. Due to massive 

westward overthrusting, the thin-skinned thrust belt has masked most of the deep seated paraauthochthonous 

platform carbonates. A SE-NW orientation anticlinorium trend of deep paraautochthonous 

platform carbonates is interpreted just north of Vlora-Diber Lineament (VDL). 

The anticlinorium, which is draping over pre-Mesozoic basement and stretched out for about 

140 km into onshore Montenegro, could hold several structural closures along strike. The 

thick-skinned structuration is mainly due to post-Oligocene inversion, coincident with post 

oligocene westward thrusting. The Kruja-Dalmatin thin-skinned ramps are draping over the 

anticlinorum and mimicking the underlying topography, in dip and strike orientation. Deep 

seated autochthonous platform carbonates in onshore western Albania region resemble the 

Southern Apennines plays in Italy, where more than 3 billion OOIP have been discovered so 

far from fractured carbonate reservoirs (Fig. 3). 

The exploration of the thin-skinned thrusts plays of the platform carbonates is considered of 

high risk mainly due to immature and insufficient Cretaceous SR to generate commercial HC 

in such levels and also of high risk on sealing capacities. The deeply buried Cretaceous SR, 

analogue to those contributed to Southern Appenines discoveries are modeled to generate the 

necessary amounts of light oils, trapped into fractured shallow water carbonates reservoirs and 

sealed by Oligocene regional seal (Fig. 4). Two major deep rooted transversal faults in the 

area known in published literature as Scutari-Pec Lineament (SPL) and Vlora-Diber 

13

Lineament (VDL) contribute in post-orogeny shaping and could also help migration of HC 

generated from nearby intra-platform basins. 

Despite the fact that the regional platform architecture setting is less studied and understood 

than the fertile Ionian basin in the south and because of discouraging results over the years, 

the future petroleum exploration efforts in this region should be diverted more and more 

towards the platform sub-thrust plays. 

Fig. 1: General view of the NW Albania – Montenegro region. Despite abundant oil 

shows in the region no discovery has been achieved so far till now. 

Fig. 2: Simplified geo-tectonic map showing the morphology between South Adriatic 

Basin and the Kruja-Dalmatian platform zones (After OMV, 2000). 

14

Fig. 3: Source rocks distribution within the Mesozoic sequence (Modified after Zappatera, 

1994). Analogue source rocks of Cretaceous age proved in Southern Appenines are 

expected in the Study Area. 

Fig. 4: Simplified regional geological section from Southern Appenines (Italy) to Krasta Zone 

(Albania) showing that deep seated autochthonous platform carbonates in onshore 

western Albania region resemble the Southern Apennines plays in Italy (Modified after 

Picha, 1995). 

15




DIGITALIZATION of DATA RELATED to the AGE of ALBANIAN OPHIOLITES 

Ariana BEJLERI 1 *, Mensi PRELA 2 , Flutura HAFIZI 3 

1 Polytechnic University of Tirana, Faculty of Information Technology, Computer 

Engineering Department, Tirana, Albania, arianabejleri@yahoo.com. 

2 Polytechnic University of Tirana, Faculty of Geology and Mining, Earth Science 

Department, Tirana, Albania, mensiprela@yahoo.com 

3 Polytechnic University of Tirana, Faculty of Geology and Mining, Earth Science 

Department, Tirana, Albania, hflutura@yahoo.com 

* Ariana BEJLERI 

The age of Albanian Ophiolites has been determined by the age of siliceous sections, lying 

above them. The aim of this study is to digitalize the data provided by radiolarian 

assemblages yielded in this siliceous sections. Radiolaria are protozoic organisms with 

siliceous shell, abundant in the sedimentary rocks lying above the ophiolites all over the 

Tethys realm. The data for the Radiolarian Assemblages in Albania are taken from the Chert 

sections which belong to the siliceous sedimentary cover of the ophiolite of the Mirdita Zone 

and to the carbonate successions deposited on the continental margin of the ophiolites. These 

data are abundant and the way that this information is available in the existing format, is not 

convenient to be easily used. In order to resolve this problem we have developed a relational 

database by applying MS Access techniques which will facilitate the use of this data from 

different users. With this program we can provide the whole information when the section or 

the sample is known, by using different queries. The whole information has been presented in 

tabular form, with the tables interacting in a very harmonious and functional relationship with 

each other. The tables contain information about chert sections in which the radiolarian 

assemblages are taken: their location, position of samples in these sections, age, lithology, 

photos etc. The tables also contain a lot of information about the radiolarian assemblages in 

every sample: list of radiolarian species, age, author, species descriptions, photo etc. We can 

also edit all this information or enter new data according to them. This database will be used 

by geologists to better understand the problems regarding the age of the beginning of siliceous 

sedimentation in different parts of Albanian Ophiolites, from north to south, from west to 

east. 

Key words: Radiolarian assemblages, Jurassic, chert, MS-ACCESS, database, section, 

species, biozonation. 

17




ANALYZING SEISMIC SITUATION in the DIBRA REGION by DIGITALIZATION 

of SEISMIC EVENTS 

Ariana BEJLERI 1 *, Flutura HAFIZI 2 , Shpresa SHUBLEKA 3 

1 Polytechnic University of Tirana, Faculty of Information Technology, Computer Engineering 

Department, Tirana, Albania, arianabejleri@yahoo.com. 

2 

Polytechnic University of Tirana, Faculty of Geology and Mining, Earth Science Department, Tirana, 

Albania, 

hflutura@yahoo.com 

3. 

Polytechnic University of Tirana, Faculty of Information Technology, Computer Engineering 

Department, Tirana, Albania, 

shubleka@yahoo.com 

* Ariana BEJLERI 

This study deals with the digitalization of the information on seismic sources in the Dibra 

region over a period of several years. By such a digitalization it is possible to present 

seismological activity in the studied region, which itself constitutes the key parameter of the 

seismic risk, which means that it is possible to identify the potential for eventual earthquakes 

in future. A great deal of analogue seismic information has been collected over years by the 

seismological network in Albania. The data show that the region has undergone several 

serious earthquakes. This is because the Dibra region is part of the strongly seismogenic zone 

of Korce-Oher-Peshkopi (Drini Alignment Zone). This is the reason why the study was 

undertaken in this region. The digitalization allows us to proceed in two main directions: first, 

to understand the seismic activity for the region, and, second, to assist in evaluating the 

expectation of eventual future seismic activity in the region. This can be accomplished by 

developing a relational and integral database. One of the main function of this database will 

be data manipulation: coordinates, time of event, magnitude, intensity, depth of source etc. 

Several queries have been established based on these data upon the request of their users and 

graphs have been also plotted, which can be updated at the moment of the data manipulation. 

Queries and graphs make possible to analyze the seismic situation in the Dibra region. This 

paper is also applicable in future research studies and is a good start, especially in precising 

the historical seismicity of our country. 

Key words: seismic situation, seismic events, Dibra region, digitalization, magnitude, 

intensity, depth of source 

19




HYDROCHEMICAL FEATURES of the KAVAJA GROUNDWATER BASIN 

(PREADRIATIC DEPRESSION, ALBANIA) 

(Poster) 

BEQIRAJ Arjan*, LUZATI Suada*, CENAMERI Majlinda* 

*Polytechnic University of Tirana, Faculty of geology and Mines ae_beqiraj@yahoo.com 

The basin of Kavaja is part of the Rrogozhina aquifer which spread out over the Albanian pre- 

Adriatic depression and extends from Shkodra in the north to Vlora in the south, over a surface of 

2100 km 2 (Eftimi, 1984). It is a multilayered aquifer consisting of intercalations between waterbearing 

Pliocene sandstone and conglomerate with impermeable clay layers. This aquifer occurs 

under typically artesian conditions because of its impermeable clay basement and semiimpermeable 

Quaternary cover. The main recharge source of the aquifer is represented by 

precipitations thanks to its vast (around 500 km 2 ) outcrop on the hilly terrains. Other recharge 

sources of the aquifer are the Quaternary alluvial aquifers on it, the rivers that intersect the 

aquifer transversally and the boundary aquifers. The groundwater shows variable geochemical 

composition due to different mineralogical composition of its medium, vast extension of the 

aquifer, variable geological and hydrogeological features, relationships with boundary aquifers 

and seawater, relations of the tested groundwater with respect to recharge and discharge zone and 

possibly the depth of wells. However, the mainly magmatic – carbonatic mineralogical 

composition of the water – bearing sandstones and conglomerates has determined a geochemical 

composition of groundwater consisting mostly of HCO3-Mg-Ca hydrochemical groundwater 

type. Such a geochemical composition characterizes the groundwater of Rrogozhina aquifer as 

chemically immature groundwater (Apelo et al., 1996), which mainly plots near the center of the 

Piper plot. Dissolution of minerals seems to be the major geochemical processes in the formation 

of the groundwater composition. Other hydrochemical types are less important and are mainly 

related with the Na enrichment in water through cation exchange processes between groundwater 

and clay formations that are more abundant over the plain extension of the aquifer. The above 

mainly magmatic composition of sandstones and conglomerates is also responsable for the high 

content of iron in the grounwater of this aquifer. Iron content is higher in sandstone related 

groundwater where the silt fraction is mainly composed by iron-bearing minerals such as 

magnetite, epidote, granate, sphene, amphibole and pyroxene. In general, the wells are drilled 

down to 250m. The general mineralization and general hardness of groundwater pumped from 

the above drilled section range from 500 to 800 mg/l and from 11 to 25ºdH, respectively. At the 

pHs commonly encountered in groundwater (pH=7.0-8.5), HCO3 - is the dominant carbonate 

species present. In general, up to the above drilled depth, all the hydrochemical parameters of the 

groundwater fit the Albanian and EU limits for the potable water. In some cases, NH4 + , SO2, Cl - , 

21

etc, are found in concentrations higher then the limits of drinking water. In the diagram (not 

shown) of Total Mineralization (TM) versus well depth (H) was found that groundwater can 

maintain TM values less that 1.0 mg/l up to a depth that ranges from 400 to 500m according to 

the well position with respect to recharge and discharge zone. 

The basin of Kavaja forms a syncline (Hyseni, 1995), whose axial part consists of water-bearing 

Astian conglomerates and sandstone covered by Quaternary alluvial sediments, whereas the 

Piacensian clay formations construct the western and eastern flanks of the syncline (Fig. 1). 

� 

Fig. 1: Geological map of the Kavaja basin 

The groundwater of the Kavaja basin belongs mostly to Ca-Mg_HCO3 hydrochemical type 

(Fig.2,3). The groundwater evolves gradually from HCO3 type to Cl type, from southeastern 

(Shkumbini river) towards northwestern (Adriatc sea) (Beqiraj et.al., 2007), that is from the 

recharge to discharge zone (Fig.4). On the other hand, the vertical evaluation of the groundwater 

geochemical composition towards the depth is expressed by means of the increase of the General 

Mineralization. Another trend of the geochemical groundwater composition, shown by gradual 

increase of the General Mineralization and Hardness (Fig. 5.a,b), is from both western and 

eastern flanks of the Kavaja depression towards its central part. The horizontal evaluation of the 

22

hydrochemical parameters of the Kavaja groundwater fits very well with the variation of the 

hydraulic conductivity values of the Kavaja aquifer. Thus, the highest values of the General 

Mineralization and Hardness correspond to the lowest values of the hydraulic conductivity. 

23

� 

Fig.�3.�Map�of�the�groundwater�hydrochemical types�� 

Fig.�2.�Kavaja groundwater�composition� 

(Piper�diagram)� 

Fig.�4.�Horizontal�variation�of�groundwater�composition 

Fig.�5.a.�Map�of�General�Mineralization Fig.�5.b.�Map�of�General�Hardness 

24 

�

� 

References� 

Appelo C.A.J. and Postma D. 1996. Geochemistry, Groundwater and Pollution. A.A. Balkema, 

Rotterdam, Netherlands. 

Beqiraj A., Hyseni A., Leka Gj and Mata M. 2007. Geological-structural aspects of the 

Rrogozhina aquifer (Albanian pre-Adriatic depression), In: abstract book of the Workshop: 

Management of Geo=mining Resources – Kosovo, 2006. P. 57. 

Eftimi R. 1984. Permeability features of Rrogozhina suite. Buletini i Shkencave Gjeologjike. 3: 

57-73. 

Hyseni A. 1995. Structure and geodynamic evaluation of Pliocene molasses of pre-Adriatic 

depression. PhD Thesis. Polytechnic University of Tirana. 175p. 

Postma D. and Brockenhuus-Schack B.S. 1987. Diagenesis of iron in proglacial sand deposits of 

late- and post-Weichselian age.�J.�Sed.�Petrology�57:�1040�1053.� 

� 

� 

25




GROUNDWATER VULNERABILITY ASSESSMENT to CONTAMINATION 

(TIRANA - FUSHE KUQE BASIN, ALBANIA) 

(Poster) 

BEQIRAJ A. 1 , PROGNI F 1 and CENAMERI M. 1 

1) Polytechnic University of Tirana, Faculty of geology and Mines ae_beqiraj@yahoo.com 

Groundwater, that represents a major source of water for domestic, industrial and agricultural 

uses in Albania, is recently suffering a deterioration of its quality especially in the regions with 

extensive demographic and industrial development. Groundwater quality has been recently 

deteriorating particularly in the basin of Tirana which represents the most contaminated one 

because of the intensive urbanization and industrialization. Groundwater vulnerability 

assessment was done by using a DRASTIC model (Aller et al., 1987) combined with a 

Geographic Information System (Arc Gis 9.2 INFO). This model has been widely used in many 

countries because the inputs required for its application are generally available or easy to obtain. 

The aim of this study is to assess the vulnerability of groundwater to contamination for the basin 

of Tirana - Fushe Kuqe basin which represents the most important alluvial aquifer of Albania 

because of high dynamic reserves and high demographic density in this region (Fig. 1). The 

main recharge occurs from the south-eastern and eastern side of the basin and groundwater flows 

to the southeastern and eastern towards northwestern and western sides of the basin. The general 

groundwater mined from this aquifer is over 4000 l/s (Puca, 2005). From the hydrochemical 

point of view, the groundwater mostly belongs to calcium – magnesium – bicarbonate type. 

Materials and Methods 

The process for the construction of the vulnerability maps involved: (i) data (hydrogeological, 

geological and pedological) collection, (ii) scanning of toposheets and digitizing (raster to 

vector) source data, (iii) creating the attribute table, (iiii) analyzing the DRASTIC factors for 

evaluation of Drastic Index, (iiiii) rating these areas as to their vulnerability to contamination and 

deriving a Graduated Map. 

The seven parameters (Depth to water (D), net Recharge (R), Aquifer media (A), Soil media (S), 

Topography (T), Impact on the vadose zone media (I), and hydraulic Conductivity of the aquifer 

(C)) that are involved in arriving at the Drastic Index have been collected from the following 

sources: Geological Survey of Albania, Institute of Soils and Institute of Topography for the 

Depth to water, Aquifer media, Hydraulic conductivity and Net recharge, Soil media, Impact of 

Vadose Zone and Topography, respectively. 

The value of Drastic Index (DR*DW +RR*RW + AR*AW + SR*SW + TR*TW + IR*IW + 

CR*CW) was calculated in Exel and was transferred to GIS 9.2 through Access. 

Results and discussion 

Different models can be applied to mapping of groundwater vulnerability, but the most 

commonly used model in assessing groundwater vulnerability in porous aquifers seems to be the 

DRASTIC model (Aller et al. 1985; Aller et al., 1987; Deichert and Hamlet, 1992,). 

27

The DRASTIC model has four assumptions (Aller et al. 1985; Aller et al., 1987): 1) the 

contaminant is present on the ground surface; 2) the contaminant is flushed into the groundwater 

by precipitation; 3) the contaminant has the mobility of water; 4) the area being evaluated by 

DRASTIC is 0.4 km 2 or larger. Higher DRASTIC index, represent a greater potential for 

pollution or a greater vulnerability of the aquifer to contamination. 

The final goal of vulnerability maps is the subdivision of the area into several hydrogeological 

units with different levels of vulnerability. As a result of the vulnerability assessment, 15% of the 

Tirana - Fushe Kuqe basin was classified as being very highly vulnerable, 10% highly 

vulnerable, 45% moderate, 15% low level and, finally, around 15% of the basin has very low 

vulnerability (Fig. 1.b). The configuration of the vulnerability to groundwater contamination fit 

very well with the data of the qualitative monitoring. This later has detected different levels of 

ammonium ions, nitrites, nitrates, phosphates, etc, in the groundwater of the southeastern sectors 

of the aquifer as it could be expected from the vulnerability map. 

References 

Aller, L., Bennett, T., Lehr, J.H., Petty, R.J., 1985, DRASTIC; A standardized system for 

evaluating groundwater pollution potential using hydrogeologic settings: Ada, OK, United 

States Environmental Protection Agency, Robert S. Kerr Environmental Research Laboratory, 

EPA/600/2-85/0108, 163 p. 

Aller L., Bennet T., Lehr J. H., Petty R. J. and Hackett G., 1987. DRASTIC; A standardized 

system for evaluating groundwater pollution potential using hydrogeologic settings: EPA- 

600/2- 87-035, 622 p. 

Deichert, L.A., Hamlet, J.M., 1992, Non-point groundwater pollution potential in Pennsylvania, 

in American Society of Agricultural Engineers (ASAE) International Winter Meeting, 

Nashville, Tennessee, 15-18 December, 1992: Paper No. 922531. 

Puca N., 2005. Scientific report: Monitoring of groundwater in the main aquifers of Albania- 

Erzeni – Ishmi aquifer. 45p. Archives of Geological Survey of Albania (in Albanian). 

�� 

28

Legend 

Well 

Fig. 1: A) Hydrographic map of Tirana - Fushe Kuqe basin; B) Vulnerability map. 

29 

A 

B




USE of CAPILLARY PRESSURE to ASSESS the FLOW-UNITS in OIL-BEARING 

CARBONATE RESERVOIRS of the ALBANIAN IONIAN ZONE 

Brunilda BRUSHULLI and Gjergji FOTO** 

Knowledge of quality of oil and gas, is one of the most important tasks of the reservoir’s 

geology. 

The study of carbonate reservoirs in Albania, has suffered from lack of information stated 

directly from samples, geophysical surveys and equipment suitable for measuring the quality 

of reservoirs. The development of oil and gas reservoirs is managed by the direct information 

but also with a high cost. 

In this paper, is presented a way to obtain valuable information from measurements of 

capillary pressure of 450 samples obtained from wells. 

The�conclusions�from�this�analysis,�already�are�validated�with�all�the�data�of�development�of� 

the�reservoirs,�and�are�more�valid�for�all�types�of�fluids,�whereas�for�carbonate�reservoirs� 

are�favorable.� 

What is a flow unit? A flow unit is a sub division defined on the basis of similar pore type. 

Petrophysical characteristics such as distinctive log character and/or porosity-permeability 

relationships, define individual flow units. Inflow performance for a flow unit can be 

predicted from its inferred pore system properties, such as pore type and geometry. They help 

us to correlate and map containers and ultimately help predict reservoir performance. (Dan 

Hartmann, Edward Beaumont, 2001p 9-7). 

Capillary pressure measurements are the tool that sheds light on the exact structure of the 

pore system, pore threat size, pore volume, etc. and therefore the flow units within reservoirs. 

Considering tests of 450 capillary pressures measurements, were noted several shortcomings 

of measurement, distribution and use of their. (Gj. Foto etc, 2007; B. Brushulli, 2008): 

To use these tests, it has been necessary to make some concessions and modifications of the 

assessment methods that are evidenced in contemporary literature, being sure that not affect 

the outcome: 

1. To assess the pore throat size from capillary pressure measurements, lacks the 

interfacial tension and contact angles of oil, consequently are used literature values 

for the general case (Dan Hartmann, Edward Beaumont, 2001 ); 

2. For determination of the Hg saturation, for each level of injected pressure, instead of 

the overall volume of porous permeable system, is used the volume of mercury at the 

higher injection pressure, 90 kg/cm 2 . 

** Faculty of Geology and Mine, Polytechnic University of Tirana, Albania; e-mail: gfoto2001@yahoo.com 

31

__________________________________________________________________________ 

This last condition, excluded the possibility to evaluating water saturation and in this case, 

the curve of mercury saturation, vs. pore throat size and capillary pressure, meet the pressures 

axis on the 90 kg/cm 2 . 

Pore throat size when mercury saturation will be 35%, will result bigger, however, retained 

relativity regarding porous structure and pore volume by their throat size. 

From visual examination of these curves and comparison with the ones known in literature 

examples (Alden J. Martin, Stephen Solomon and Dan Hartmann, 1997) seems that they can 

be grouped into four types (Figure 1 and 2) : 

Presioni i injektimit,Pk(atm) 

Presioni i injektimit,Pk(atm) 

10 2 

10 1 

10 0 

4658 49 63 

10 

0 0.2 0.4 0.6 0.8 1 

-1 

10 2 

10 1 

10 0 

Tipi ' A ' 

Tipi " B" 

73 

72 

10 

0 0.2 0.4 0.6 0.8 1 

-1 

Ngopshmëria me ujë,Su(%) 

TIPA TE LAKOREVE POROMETRIKE 

Apparently, the four types, have these features (Figure 2): 

0.1 � 

0.5 � 

2 � 

10 � 

0.1 � 

0.5 � 

2 � 

10 � 

10 

0 0.2 0.4 0.6 0.8 1 

-1 


10 2 

10 1 

10 0 

10 2 

10 1 

10 0 

Tipi ' C' 

Tipi ' D' 

6061 50 

10 

0 0.2 0.4 0.6 0.8 1 

-1 

Ngopshmëria me ujë,Su(%) 

Meso Mikro Nano 

0.1 � 

0.5 � 

2 � 

Makro 

10 � 

Mega 

Mega Makro Meso Mikro Nano 

0.1 � 

0.5 � 

2 � 

6669 10 � 

Type A, has a porous structure of throat size from megaporte type (> 10 micron), which 

provides a saturation to over 80-100% of relative pore volume, with around 1atm injection 

pressures. 

Type B, has a porous structure of the throat size from megaporte (> 10 micron), which 

provides about 50% saturation of the relative pore volume, with 1 atm. injection pressures. 

Type C, has a porous structure of the throat size in order macroporte (20-10 micron), which 

provides a saturation of about 35% of relative volume pore, with about 1atm injection 

pressure. 

Type D, has a porous structure of the throat size in order macroporte (20-10 micron), which 

provides a saturation of about 5% of relative volume pore, with about 1atm injection 

pressure. 

In this group, we believe that absent a curve of a rock that is evidenced indirectly but that can 

not handle with core and after Lucia's classification (1983), included at the type of touching 

vugs as fracture and breccias. 

32

__________________________________________________________________________ 

Considering the distribution of curves types to specific reservoirs, result very interesting 

conclusions that are proved along many years performance of reservoirs. These data are 

presented in table 1. 

REZERVOIR T Y P E O F C U R V E S 

A B C D 

Ballsh 6.6% 12% 44% 37.35% 

Cakran-Mollaj 6% 14.7% 60.5% 18.30% 

Gorisht-Kocul 8% 21.3% 29.3% 41.3% 

Probabilityi per curve 

type 

6.85% 15.7% 48.3% 29.1% 

Probability 6.85% 22.55% 70.85% 99.95% 

Eng. Brunilda BRUSHULLI, 

September 2008 

The confrontation of these data with well logs, appropriate age and their depth in Gorishti- 

120 well, (figure 3), (Table no.2), prove at general point of view, a relative good accordance 

between lithology, age and type of capillary pressure curve, and a accordance with the 

conclusions of macroscopic studies of the samples taken from wells and superficial analogues 

(Gj. Foto, 1991). In literature, isn’t clearly stated and necessity of this accordance. 

Table no. 2 

Interval TG-G G-GF >GF 

Age Eocene Paleocene-Upper 

Cretaecous 

Lower Cretaecous 

Thickenis, m 175 251 >100 

Interval 

samples 

of 43 28 4 

Type of curves per interval 

Type Numbe % Type Numbe % Typ Numbe % 

r 

r 

e r 

A 1 2 A 5 18 A - - 

B 7 16 B 7 25 B 3 75 

C 16 38 C 2 7 C - - 

D 18 43 D 14 50 D 1 25 


33

__________________________________________________________________________ 

THELLESIA E BALLIT TE PUSIT NGA REPERI "G" 

THELLESIA 

80 

60 

40 

20 

0 

20 

40 

60 

80 

100 

120 

I 

II 

NENZONA 

III 

NUMRI I PUSEVE 

TE TESTUAR 

16 1 15 6,2593,75 

14 

12 

10 

1 1 3 7 ,1 4 92,86 

2 10 16,6 83.4 

4 

6 40 6 0 

6 

5 

1 

83 17 

10 9 1 9 0 1 0 

4 

R E Z U L T A T I I PROBABILITETI 

P E R V E T E S IM IT 

POZITIVE 

3 

1 

(+ ) (-) 

75 25 

4 3 1 75 25 

Figura 37 Sipas Gj. Foto 1991 

R E Z U L T A T E T E P E R V E T E S I M I T 

R E Z E R V U A R I I A M O N IC E S 

NEGATIVE 

2 2 0 100 0 

Testing results vs depth 

Eng. Brunilda BRUSHULLI, 

September 2008 

P R O B A B IL IT E T I I 

PERVETESIMIT POZITIV 

20 40 60 80 % 

Punoi: B. Brushulli 

These conclusions are in accordance with dynamic data of reservoir, and that are presented in 

the study of the distribution of positive tests of wells versus the depth in Amonica reservoir 

(Figure 4). 

Seems clearly a very good accordance of all data and qualitative evidence of flow units that 

can be effectively used for development of new reservoirs and their mapping in the Ionian 

Zone of Albania. 

References 

Alden J. Martin, Stephen Solomon and Dan Hartmann, 1997- Characterization of 

Petrophysical Flow Units in Carbonate Reservoirs; AAPG Bulletin, V. 81, No.5 (May 

1997), p.734-759. 

Dan Hartmann, Edward Beaumont, 2001- Predicting Reservoir System Quality and 

Performance; in Exploring for Oil and Gas Traps, edited by E. Beaumont, N. Foster. 

F. Jerry Lucia, 1983- Petrophysical parameters estimated from visual description of 

carbonate rocks: a field classification of carbonate pore space: Journal of Petroleum 

Technology, March, v.35, p. 626-637. 

F. Jerry Lucia, 1995-Rock-Fabric/Petrophysical Classification of Carbonate Pore Space for 

Reservoir Characterization; AAPG Bulletin, V.79 (September 1995), p.1275-1300. 

Francois Roure, Shaqir Nazaj, Kristaq Muska, Ilia Fili, Jan.P. Cadet, M. Bonneau. 2003 - 

Kinematic Evolution and Petroleum System: An appraisal of the outer Albanides. 

Key Words: oil & gas; reservoir, flow unit, capillary pressure, pore & throat size 


34 

55




IMPACT of SINGLE FAULTS on the FLUID FLOW and HEAT TRANSPORT: 

FIRST RESULTS from 3D FINITE ELEMENT SIMULATIONS 

Yvonne CHERUBINI a,b , Mauro CACACE a,b , Magdalena SCHECK-WENDEROTH a , 

Mando Guido BLOCHER a,c , Björn LEWERENZ a 

a Helmholtz Centre Potsdam - GFZ German Research Centre for Geosciences, Telegrafenberg, 

D-14473 Potsdam, Germany (yvonne.cherubini@gfz-potsdam.de) 

b University of Potsdam, Am Neuen Palais 10, D-14469 Potsdam, Germany 

c Brandenburg University of Technology, Konrad-Wachsmann-Alle 1, D-03046 Cottbus, 

Germany 

Fractures and faults are likely to have a significant impact on the solute, fluid and heat 

transport in the subsurface. Depending on their hydraulic properties, faults can act either as 

preferential pathways or as barriers to fluid flow. 

To investigate the influence of faults on the hydrogeothermal field, simulations of the 3D 

coupled fluid and heat transport are carried out. Such models allow to quantify the effects of 

different fault geometries and physical rock properties on the temperature distribution. 

In general, it is a challenging task to represent the geometry of complex fault systems 

including dipping and intersecting fractures within a permeable matrix in a 3D numerical grid. 

Thereby, it is crucial first to understand the impact of single faults on the fluid and heat 

transport before modelling more complex structural settings. 

These numerical models with simple fault geometries involve variations in fracture size, 

orientation, aperture and variable physical rock properties. 

The faults are numerically represented as 2D discrete surfaces within a 3D tetrahedral 

volume. For the Finite Element simulations we use the numerical simulator Open 

Geosys/Rockflow (Kolditz et al., 2003). Based on this approach, first results from modelling 

of simple fault systems in different geological settings are presented. 

References 

Kolditz, O., deJonge, J., Beinhorn, M., Xie, M., Kalbacher, T., Wang, W., Bauer, S., 

McDermott, C., Kaiser, C.I., Kohlmeier, R., 2003. ROCKFLOW Theory and User 

Manual, release 3.9. Tech. rep., Groundwater Modeling Group, Center for Applied 

Geosciences, University of Tübingen & Institute of Fluid Mechanics, University of 

Hannover. 

35




AIMS and PERSPECTIVES of ILP and TOPO-EUROPE 

Pr. Dr. Sierd CLOETINGH, VU-Amsterdam 

sierd.cloetingh@falw.vu.nl 

ILP stands for Integrated Solid Earth Sciences in its broadest sense. 

The lithosphere is THE connection between deep Earth and surface processes. Lithospheric 

studies, therefore, are a natural bridge between, for example, geophysics, geology and 

geomorphology. The study of the lithosphere deals with fundamental aspects of system Earth, 

and how the underlying processes operate. At the same time, lithospheric research holds the 

key for a better understanding of the controls on the occurrence of natural resources and 

environmental hazards. Sedimentary basins, being the site of mankind largest energy and 

fresh water resources, are, by their nature, an extremely effective interface between Academia 

and Industry. Quantitative modelling has made important progress during the last decade. At 

the same time, it is vital to constrain and test these models trough an array of high quality 

geological and geophysical data sets. 

ILP has initiated a large number of task forces and regional coordinating committees to 

facilitate the dialogue and exchange of information needed for further progress in integrated 

Solid Earth Sciences. The Task Force on Sedimentary Basins is a flagship of ILP. The 

regional coordinating committee TOPO-EUROPE is exemplary for this integrated Solid Earth 

approach at the scale of a continent and its margins, linking for instance sediment source-sink 

dynamics. 

Continental topography is at the interface of deep Earth, surface and atmospheric processes. 

Topography influences society, not only as a result of slow landscape changes but also in 

terms of how it impacts on geohazards and the environment. When sea-, lake- or groundwater 

levels rise, or land subsides, the risk of flooding increases, directly affecting the 

sustainability of local ecosystems and human habitats. On the other hand, declining water 

levels and uplifting land may lead to higher risk of erosion and desertification. In the recent 

past, catastrophic landslides and rock falls have caused heavy damage and numerous fatalities 

in Europe. Rapid population growth in river basins, coastal lowlands and mountainous regions 

and global warming, associated with increasingly frequent exceptional weather events, are 

likely to exacerbate the risk of flooding and devastating rock failures. Along active 

deformation zones, earthquakes and volcanic eruptions cause short-term and localized 

topography changes. These changes may present additional hazards, but at the same time 

permit, to quantify stress and strain accumulation, a key control for seismic and volcanic 

hazard assessment. Although natural processes and human activities cause geohazards and 

environmental changes, the relative contribution of the respective components is still poorly 

understood. That topography influences climate is known since the beginning of civilization, 

but it is only recently that we are able to model its effects in regions where good (paleo-) 

topographic and climatologic data are available. 

37

TOPO-EUROPE addresses the 4-D topographic evolution of the orogens and intra-plate 

regions of Europe through a multidisciplinary approach linking geology, geophysics, geodesy 

and geotechnology. TOPO-EUROPE integrates monitoring, imaging, reconstruction and 

modelling of the interplay between processes controlling continental topography and related 

natural hazards. Until now, research on neotectonics and related topography development of 

orogens and intra-plate regions has received little attention. TOPO-EUROPE initiates a 

number of novel studies on the quantification of rates of vertical motions, related tectonically 

controlled river evolution and land subsidence in carefully selected natural laboratories in 

Europe. From orogen through platform to continental margin, these natural laboratories 

include the Alps/Carpathians-Pannonian Basin System, the West and Central European 

Platform, the Apennines-Aegean-Anatolian region, the Iberian Peninsula, the Scandinavian 

Continental Margin, the East-European Platform, and the Caucasus-Levant area. TOPO- 

EUROPE integrates European research facilities and know-how essential to advance the 

understanding of the role of topography in Environmental Earth System Dynamics. The 

principal objective of the network is twofold. Namely, to integrate national research programs 

into a common European network and, furthermore, to integrate activities among TOPO- 

EUROPE institutes and participants. Key objectives are to provide an interdisciplinary forum 

to share knowledge and information in the field of the neotectonic and topographic evolution 

of Europe, to promote and encourage multidisciplinary research on a truly European scale, to 

increase mobility of scientists and to train young scientists. 

References 

Cloetingh S. and Negendank, J. (Eds.), 2010. New Frontiers in Integrated Solid Earth Sciences. 

Springer Verlag, p.1-412. 

Cloetingh S., Thybo H., Faccenna C. (Eds.), 2009. TOPO-EUROPE: The Geoscience of 

coupled Deep Earth-surface processes. Tectonophysics, Special issue, v. 474, p. 1-416. 

Cloetingh S., Ziegler P., Bogaard P., Andriessen P., Artemieva I., Bada G., Balen van R., 

Beekman F., Ben-Avraham Z., Brun J.-P., Bunge H.-P., Burov E., Crabonell R., Facenna 

C., Friedrich A., Gallart C., Green A., Heidbach O., Jones A., Matenco L., Mosar J., 

Oncken O., Pascal C., Peters G., Sliaupa S., Soesoo A., Spakman W., Stephenson R., 

Thybo H., Torsvik T., Vicente de G., Wenzel F. and Wortel M., 2007. TOPO-EUROPE: 

The geoscience of coupled deep Earth-surface processes. Global and Planetary Change, 

v. 58, p. 1-118. 

Lacombe O., Lavé O., Roure F. and Vergés J., eds, 2007. Thrust belts and foreland basins: 

From fold kinematics to hydrocarbon systems. Frontiers in Earth Sciences, Springer, 

492 pp. 

Roure F., Cloetingh S., Scheck-Wenderoth M., Ziegler, P.A., 2010. Achievements and 

challenges in sedimentary basin dynamics: A review. In: New Frontiers in Integrated 

Solid Earth Sciences (Ed. by S. Cloetingh and J. Negendank). Springer-Verlag, p. 145- 

233. 

Scheck-Wenderoth M., Bayer U. and Roure F., guest editors, 2008. Progress in understanding 

sedimentary basins. ILP Task Force, Special issue of Tectonophysics. 

38




A CASE STUDY on PROBALISTIC EVALUATION 

of SOIL LIQUEFACTION 

Shkëlqim DAJA, Polytechnic University of Tirana, Faculty of Geology and Mining, Albania, 

daja_s@yahoo.com 

Neritan SHKODRANI, Polytechnic University of Tirana, Faculty of Civil Engineering, Albania, 

neritans@yahoo.com 

In this paper the liquefaction potential of Quaternary soft non-cohesive soils has been assessed. 

Generally, liquefaction will occur in loose clean to silty sands that are below the groundwater 

table, of Holocene age situated in a maximum depth of 20 m below the ground surface. This 

assessment is based on the engineering characteristics of the seismic hazard expressed in terms 

of Peak Ground Acceleration at the bedrock and 5% Damped Elastic Response Spectra for rock 

and soil conditions. The approach followed for the analysis is the probabilistic one, which means 

that engineering characteristics of the shaking are estimated for a certain probability of 

occurring. The liquefaction vulnerability has been computed considering the hazard level 

corresponding to different levels of safety, such as 10% in 10 years (72-years Return Period), 

10% in 50 years (475-years RP) and 2% in 50 years (2475-years RP). The seismological data 

used in the analyses contains earthquakes with MS 4.5 and covers a time span from 58 up to 

2009. The calculation of cyclic resistance ratio (CRR) and the cyclic stress ratio (CSR) of the 

soils are based on SPT (Standard Penetration Test) values. 

Keywords 

Liquefaction evaluation, probability, earthquake, cyclic resistance ratio, cyclic stress ratio, 

safety factor. 

References 

1. Riga G., 2008. “Microzonazione sismica: Procedure per elaborare una carta di 

pericolosità sismica”, 268. 

2. Seed, H. B., Tokimatsu, K. Harder, L. F., and Chung, R. M., 1985. Influence of SPT 

procedures in soil liquefaction resistance evaluation. Journal of Geotechnical Engineering, 

ASCE, 111 (12), 1425-1445. 

3. Sulstarova E., Kociu S., Muco B., and Peci B., 2005. Catalogue of Earthquake in Albania 

with MS � 4.5 for the period 58-2004. Internal Report, Seismological Institute, Tirana. 

4. Takada T., 2006. Hand Calculations of Seismic hazard Curve. Lecture notes, University 

of GRIPS, Japan. 

5. Aliaj SH., Adams J., Halchuck S., Sulstarova E., Peci V., and Muco B., 2004. 

Probabilistic Seismic Hazard maps for Albania. 13 th World Conference on Earthquake 

Engineering Vancouver, B.C., Canada, 13. 

6. Kramer S., 1996. Geotechnical Earthquake Engineering. Prentice Hall, New Jersey, 653. 

39




The ROLE of GEOLOGICAL FACTOR in the CHEMICAL CONTENT of the 

QUATERNARY GRAVEL AQUIFERS of the PREADRIATIC DEPRESSION 

(Poster) 

Dr. Elsa DINDI 

Geology and Mining Faculty 

Department of Geoinformatics, Applied Geology and Environment 

E-mail: edindi@yahoo.com 

In natural conditions, chemical composition of underground waters is consequence of 

many factors of physical, chemical, biological, geographical, geological, hydrogeological 

and anthropogenic nature. 

In determined conditions one of this factors takes the main importance, the others give 

their influence indirectly. Geological factor influences in to directions: lithological and 

tectonically ones. 

Considering in this way, the lithological factor plays the direct role and tectonic plays the 

indirect one. 

The role of lithological factor, in Preadriatic Depression gravel Quaternary aquifers, has 

conditioned some common characteristics related to mineralogical composition of the 

gravel which is reflected to the chemical composition of the ground waters. 

The role of tectonics has conditioned indirectly the physical, hydrogeological and 

hydrodynamic features of these aquifers, witch in their own part plays role in spatial 

evolution of chemical composition of underground waters. 

Tectonic factors have conditioned some common features for gravel quaternary aquifer of 

Mati River, Tirane-Ishem-Erzeni aquifer and Vjosa River aquifer. Gravel quaternary 

aquifer of Lushnja represents different features comparing to mentioned aquifers. 

Tectonics has conditioned the spatial extension of these aquifers representing some 

common characteristics, such as: 

� Increasing of top cover clay from eastern to the western part of the aquifers. 

� Increasing the content of sand comparing to gravel, toward the west, influencing 

directly on the hydrogeological parameters of the aquifers. 

� Increasing the thickness of the aquifers toward the west. 

� The movement of ground waters is from Southeast to Northwest (except Lushnja 

gravel aquifer, where this direction is from North to South, and from East and West to the 

Center). 

� Spatial changes in chemical composition of ground waters. 

Closed to the recharge areas ground water belongs to HCO3 type, influenced by the 

chemical composition of river waters. Changes take place toward the west: increase TDS, 

ion HCO3 decreases, ion Cl increases etc... 

41

This common or different characteristics of Preadriatic Depression gravel Quaternary 

aquifers are presented in hydrogeochemical maps and cross sections. 

Keywords: aquifer, tectonics, ground water chemical composition, Preadriatic 

Depression. 

References 

Aliaj Sh., 1998. Neotectonic structure of Albania. The Albanian Journal of Natural & 

Technical Sciences, No. 4. 

Aliaj Sh., 2000. Map of the active faults in Albania, at scale 1:200 000. Seismological 

Institute, Academy of Sciences, Tirana. 

Babameto A., 1978. Hydrogeology of Fushe Kuqe well field snd the possibility of Durres 

city supply,(in Albanian)Albanian Hydrogeological Survey, Report Tirana. 

Dindi E., 2009. “Some considerations on the water quality of the aquifer on the down 

stream of Erzeni River valley”, “Buletini i Shkencave Teknike”. 

Dindi E., 2009. Phd thesis “Management and sustainable exploitation of ground water 

recourses of Vlora area”. Faculty of Geology and Mining, UPT. 

-Eftimi, R. 

“Ujra nentokesore te zones se Lushnjes”: permbledhje studimesh (Groundwater of the 

Lushnja area: summaries of studies (in Albanian). 

Albanian Hydrogeological Survey, Tirana, 1975, Albania 

-Eftimi, R. 

Karakteristikat filtruese dhe aspekte gjeologjike të shtresave ujëmbajtëse ne Shqipëri 

(Filtration characteristics and geological aspects of the aquifers in Albania, in Albanian). 

Albanian Hydrogeological Survey, Tirana, 1982, Albania 

- Eftimi, R., Tafilaj I. (1996) 

Groundwater of Erzeni-Ishmi Rivers basin. In water resources management of Erzeni- 

Ishmi Rivers basin. 

Priority action programme. Regional activity center, Split, Kroacia. Word Bank. 

-Fetter C.W. 

Applied Hydrogeology, third edition, New Jersey,07458. 

-Group of authors 

Geological map of Albania, at scale: 1:200.000, Tirana, 2004. 

-Group of authors, 

Albanian Hydrogeological Survey 

Hydrogeological Map of Albania. at scale: 1:200.000, Tirana 1985, Albania 

-Strazimiri, D.L. and Motz, L.H.(1997) 

Groundwater flow model of the northern part of the Lushnja aquifer in Albania. 

Hydrological Sciences Journal, 42: 5, 679-69 

-Tafilaj I., Dindi E., Saraci M.(2000-2002) 

“Management of territory and natural resources on the area Tirane-Durres-Kavaje (in 

Albanian). 

Albanian Hydrogeological Survey. Sub. Project 1.1. “Groundwater resources”. 

42




SEQUENCE STRATIGRAPHIC of DEEP-WATER SERRAVALLIAN 

SILICICLASTICS of the ZVERNECI OUTCROP - VLORA REGION-ALBANIA 

Prof. Dr. Çerçis DURMISHI 

Polytechnic University of Tirana, cecodurmishi@yahoo.com 

Despite the numerous studies carried out around the world in the last 30 years on both modern 

and ancient deep water siliciclastic systems, the level of knowledge is continually evolving. 

A wide variety of siliciclastic systems are found in modern and ancient basins and their differing 

characteristics of sedimentation and the complex interplay of such factors as paleogeography, 

paleo-topography, bathymetry, catastrophic events, regional basin development and sedimentary 

sources have still not been adequately explained. Neither the sedimentological fan model 

(Normark,1970; Mutti and Ricci Lucchi,1972; Walker,1978), nor the “eustatic” sequencestratigraphic 

model (Posamentier et. al,1991) adequately describe the great variety of deep-water 

siliciclastic systems. 

The sedimentary model proposed for the Serravalian of this region is a “hybrid” deep water 

siliciclastic system. This “hybrid” model contains elements of both classical and modern systems 

which have been proposed by various authors. It also presents some unique characteristics which 

are observed in both the vertical and horizontal directions. 

Recent studies concerning the sedimentology of other regions of molasse deposits within the 

peri-Adriatic Depression of Albania are expected to complement the model proposed in this 

study. 

The description of this model will contribute to the understanding of the deep water sediments 

within the basin and will form the basis for a detailed petroleum exploration model. 

The Serravalian deposits in the Zverneci outcrops are part of a foredeep basin in the most 

southern margin of the molassic Periadriatic Depression of the South Adriatic region. 

These sediments are characterized by three major depositional sequences: 

Sequence I- Slope deposits. 

Sequence II- Middle-fan, fan complex deposits. 

Sequence III- Slope deposits. 

Total sediment thickness is more than 1800m. 

A pre-dominantly NW-SE(AZ 340 grade) trend for the sediment source direction has 

been established. Three possible source areas (Tragjas-Dukat, Bolene-Terbac, and the 

Sevasteri area) are interpreted to have contributed sediments to deposition in the Zverneci 

area. 

The depositional environment is characterized by lowstand deep-water siliciclastic 

systems of turbidite facies.Fan Complexes, supra fan lobes and slope sediments are seen. 

The main turbidite elements are fan complexes consisting of channels, channel-lobe 

transitions, fan lobes, channel-margins and overbank facies. 

43

The gross lithologies observed are sandstones, siltstones, turbiditic shales and 

hemipelagic marls. 

Sandstone reservoirs: channels, lobes and channel-lobe complexes display reservoir 

quality with 25%-30% porosity. The sands, mainly quartzitic-feldspathic in character, 

have thicknesses varying from 0.5m-10m. 

Four main facies types can be distinguished within the Zverneci outcrop section: 

Facies A- Massive turbidite sandstones(thickness 0.5m-10m). 

Facies B- Thin-bedded turbidites (thickness 0.5 m- 15 m) 

Facies C- Turbiditic shales (thickness 0.5 m – 6 m) 

Facies D- Hemipelagic marls ( thickness 0.2 m- 20 cm) 

Both high-density turbidity current (HDTC) and low-density turbidity current (LDTC) 

transportation mechanisms are present in the area. 

44




SPECTACULAR EVIDENCE of SEDIMENTARY STRUCTURES of the SERRAVALIAN 

DEPOSITS in the ZVERNECI OUTCROPS (ALBANIA) 

� 

Prof. Dr. Çerçis DURMISHI, Polytechnic University of Tirana, Albania, cecodurmishi@yahoo.com 

Dr. Shkëlqim DAJA, University Polytechnic of Tirana, Albania,daja_s@yahoo.com 

Keywords: Serravalian deposits, turbidity environment, Sedimentary structures: flute casts, groove 

casts, prod casts, bounce casts, tool casts, Load casts, Flame structures, Rip-up clasts, Biogenic 

Structures/Trace Fossils. 

The Serravalian deposits in the Zverneci outcrops are part of foredeep basin in the most southern 

margin of the molassic Periadriatic Depression of South Adriatic region. 

Sedimentary structures observed in the Zverneci outcrop have been classified in 6 groups: 

A. Paleocurrent Indicators 

A.1. Bedding top structures: 

Directional sedimentary structures on the sandstone beds on the Zverneci outcrop are mainly symmetric 

and asymmetric ripple marks. The ripple marks are present on the top of each sandstone bed. Their 

spectacular presence has caused many geologists to doubt the turbidity environment of the 

sedimentation of these deposits. One possible explanation is that their presence on the top of every 

sandstone bed is a result of the current waves which are always created after every turbidity pulse moves 

the mass of sediment into the basin. In this case these current waves are almost perpendicular with the 

direction of the turbidity pulsations, (see: Direction of paleocurrent). 

A.2. Base bedding structures. 

Bed floor directional groups are present on the Zverneci outcrop. The well preserved and pervasive 

nature of these features has facilitated the compilation of a comprehensive database of paleocurrent 

measurements. These groups are present along the axis at the base of each depositing fan. Most common 

are: flute casts, groove casts, prod casts, bounce casts, tool casts; 

Flute cast: There is a presence of large and small flute casts; composite corkscrew flute cast and 

elongate flute cast. The flute casts of the elongate and flat type may be observed at the upstream end of 

the deposition, whereas the corkscrew type forms downstream: 

coalescent flute casts 

the composite flute cast is formed by the linear grouping of overlying elements the elongate flute cast is 

pointed upstream note the presence of the flat flute cast with a conical upstream termination note the 

spiraled flute cast triangular flute casts are arranged in line and superposed arched lute cast sharp 

upstream extremity. It may be assumed that the rectilinear upstream sections corresponds to hollowing 

out by a more or less linear current whereas the raised section represents an eddy area from which the 

current diverges 

Groove cast: Note that it is serrated lengthwise and appears on the inner surface of a sequence 

commencing with sands b. Also note the fine linear groove casts. 

Tool casts a large number of tool casts. 

B. Deformation structures 

Deformation structures are common in outcrop. These structures are found mainly on the base of thick 

sandstone sequences but also inside massive sandstones. 

Load casts: A load cast cutting shows general graded-bedding with a rather clear break in granulometry 

between the proper fill and the load casts and the sequence body: globular, mushroom-shaped load cast 

well-marked, large globular load casts load structures at the base of the fan deposits (channel and lobe) 

45

Flame structure:. Flame shaped structures are prevalent on the Zvemeci outcrop. There are large and 

small flame structures. These structures are formed during (penecontemporaneously) sedimentation 

and are closely related to the convolute structures. These are the result of the fluid escape under the 

pressure created by the weight of overlying sediments. 

C. Forced sedimentary structures. 

Two types of "forced" structures have been observed: 

a. - "moving force" 

b.-" circled force" 

These features are created when turbidity pulses encounter natural barriers within the basin which serve to 

deflect the flow of sediment thus creating 'circular' geometries. 

D. Rip-up clasts 

Rip-up clasts are a dominant feature of the Zvemeci outcrop. Their occurrence at the base of or within 

the sandstone units is a meaningful indicator of the following sedimentologic processes: the high 

energy of the depositional pulses: the high degree of erosion of the underlying sediments (mainly clay 

facies), the density of turbidity pulses, the shale clasts are products of intrabasinal erosion, shale clasts 

may have a negative impact on reservoir quality. 

E. Biogenic Structures/Trace Fossils 

Trace fossils are found in the upper part of the sequence within thin and rhythmic sandstone beds 

deposited under lower energy conditions. The specific ichnofacies observed are listed below: 

Zoophvcos and Nereites Typical fossil trace 

Zoophycos ichnofacies: 

(bathyal zone) Zoophycos 

Nereites ichnofacies: Helminthoida 

(Abyssal zone) Cosmorhaphe 

Taphrhelminothpsis. 

F. Concretions 

Sandstone concretions are present on different levels within the sequences. The detailed observations 

reveal that the nuclei of these concretions are comprised of marls of Burdigalian age. This suggests 

movement of turbidity currents along the top of Burdigalian marls as an initial erosional 'pulse'. 

REFERENCES 

DURMISHI.Ç. et.al.,1993. Manuali I Sedimentologjise: Figurat dhe gjeometria e trupave sedimentare 

copezore te ultesires Pranadriatike. 100 faqe, Botimi i Projektit TEMPUS, ORSAY-PARIS 

(Fond i Seksionit te Petrologjise dhe Sedimentologjise). 

DURMISHI.Ç., 1994. Albania. study: the sedimentation environment of Plio-Miocene deposits of 

Periadriatic Depression. Fondi; O.M.V. (Albanien) Exploration Ges. m.b.H. Tirana. 

DURMISHI.Ç., 1995. Turbidite environment of Plio-Miocene deposits of the Periadriatic Depression 

(Albania. Poster, Kongresi i 5-te i Sedimentologeve Franceze dhe Mitingu i 16-te i 

Sedimentologeve Europiane, Aix-lesBains-France. 

DURMISHI.Ç., 1997. Sequence stratigraphy and reservoir characterization of deep-water Serrevalian 

silicoclastics of the Vlora Region-Albania. O.M.V. (Albaniea) exploration Ges.m.b.H. Tirana. 

DURMISHI.Ç, MELO V. et.al., 1999-2001. Identifikimi dhe vleresimi i potencialeve unikale te 

gjeotrashegimnise dhe menaxhimi i vlerave te tyre gjeoturistike. Lokale, Kombetare dhe 

Nderkombetare te Shqiperise. Programi Kombetar i Zhvillimit,MASH,Tirane. 

MEÇO S, STRAUCH.F., DURMISHI.Ç. et.al.., 2004. Die Molassen der jungen Faltrengebirge 

Albaniens.Munstrsche Forschungen zur Geologie und Palaontologie.Heft 99. 

46




KINK BANDS and CHEVRON FOLDS CHARACTERISTICS of the SARANDA ANTICLINE: 

ESTIMATION of the "GEOLOGIST's MOSAIC", SOUTH-WESTERN ALBANIA 

Prof. Dr. Çerçis DURMISHI, Polytechnic of Tirana, Albania, cecodurmishi@yahoo.com 

Prof. Vangjel MELO, Polytechnic of Tirana, Albania 

Ing. Ervin LULA, Island International Exploration BV-Albania. elula@islandoilandgas.com 

Observations of events leading to development of kink bands, their origin, and changes in their 

morphology are recorded during the deformation in the "Geologist's mosaic" 1 ' in southern Albania. 

Kinking in natural deformed limestone strata has been investigated to determinate the complete history, 

of this deformation during the Paleocene. A model is presented to show in general terms the 

characteristics of these types of folds and also to explain the origin of observed kink. 

Key words: Tectonic, Kink Bands, Chevron Folds, dome-brachianticline, Ionian Zone, Paleocene, 

clay-siliceous-carbonate beds 

"GEOLOGIST'S MOSAIC" 

The purpose of this poster is to qualitatively and quantitatively analyse an outcrop with kink bands in southern 

Albania (nearby the city of Saranda), to place this particular deformation feature into its local and regional 

context, to discuss the structural and tectonic significance of kinking and to explain the tectonic conditions in 

which kinking occurs in the study area. 

In the geological interpretation and aspect this "MOSAIC" represents a complication dome-brachianticline in the 

western flank of the Saranda anticline. This section viewed as an asymmetric anticline. The south-eastern flank 

has a gentle dipping (about 25° - 30°), while the north-western flank has steepness bigger then that, almost 

vertical (Fig. 1). 

In terms of geological setting this section is of Paleocene in age. Mostly, the centre of the structure is covered 

as a "roof from a thick turbidite horizon, which uncovered in the south-western flank of the mosaic. The 

carbonate strata are represented from thin-bedded limestones with reddish and/or greenish cherty intercalations 

few centimetres thick and from very thin clay-siliceous-carbonate beds. 

The difference in thickness between turbidite limestone strata which have been repeated in the section and 

which has a thickness of 1 - 2 meters (competent layer), and thin limestone layer of about 0.4 meters 

(incompetent) strata with cherty intercalations which are also dominant in the section, have been created a 

kink bands and chevron folds mosaic inside this section with different shapes, and with a moderate ratio "n" (n 

= d2/di, di = competent layer; d2 = incompetent layer). The estimation of the shortening for the whole structure, 

caused by the "megakinks" is between 33% and 36%. These kink bands and chevron folds are not characteristic 

for the turbidite limestone strata, which has been as boundaries inside of which have been developed the 

disharmonic microfolds. 

Geometric characteristic of the microfolds are very different, they change in the south-eastern flank of the 

mosaic, in the core, north-western flank as if from the top to the bottom of the mosaic. 

The south-eastern flank of the mosaic is less affected from the kink bands. This flank, which has a gentle 

dipping and could have been affected by the tectonic press or even extension, that caused non-development of 

the typical microfolds but just some flexural slips and some kink bands. If it will supposed that both of the 

turbidite horizons where thin carbonate strata it's attached, will move up and down, the stress create a 

orientation when the shear stress acted as a band and create the kink bands. 

47

----------------------------------------------------------------------------------------------------------------------------------- 

1. The term "Geologist's mosaic" was used (DURMISHI Ç.) in the National Conference of Geology, Tirana 

2000. 

A 

B 

FIGURE 1.General schematic view of the “GEOLOGIST’S MOSAIC” 

Another reason could be also the fact that, in this flank the thick turbidite strata is imposing its folding style to 

the thin carbonate strata, that should not been microfolded. This could be the case, because we can see in the 

top of the strata and even in the northwestern flank of the mosaic, nearby these horizons that there is not an 

intensive development of the microfolding. 

48 

C

The north-western flank and the centre of the mosaic are complicated with a large amount of the kink bands. 

The hinge area in these folds is sharp and the limbs are getting directly connected at the hinge. 

In the top of the mosaic, just below to the turbidite strata, folding are rarely compare to the bottom part of the 

mosaic from the effect of the turbidite horizons. 

In the limbs of the most well developed kinks, are seen some microfolds, the limbs of which are continuing 

almost horizontal in direction (bottom - up) of the turbidite horizon. 

The kinks in their sharp part has the tendency to extend the "angle", while the thickness, mostly in the ductile 

strata is getting bigger and in some places gives the impression of saddles. 

In the centre of the mosaic are also seen few folds with the shape of the M-letter, which could have been the 

effects of the horizontal forces that can be acted over there. 

In the western flank of the mosaic, nearby the centre have been developed some box folds, but they have 

very gentle dipping axial plane to the bottom of the section, almost convex the upper limb, but with vertical 

or overturned the lower limb. 

All these folds are linked with the stress tectonic regime which have been occurred later, with the force 

orientation in oblique manner or along the layering of the hole anticline structure of Saranda with normal stress 

oriented from southeast - northwest which in the framework of structuration of the Ionian zone, create also the 

structure of Saranda. 

Some of the conclusions over the stress fields acted in the area under investigation are presented below: 

� Phase of the carbonate and flysch accumulation during Mesozoic to Aquitanian. Stress field could 

have been in extension with the orientation east-northeast - west-southwest if later there was no 

rotation. 

� Lower Miocene, before the Burdigalian. Compression and folding, which will have been, placed the 

Burdigalian with angular unconformity over the flysch. 

REFERENCES 

Baronnet, A. and Olives, J., 1983. The geometry of micas around kink band boundaries I. A crystallographic 

model. Tectonophysics, 91: 359-373. 

Bega, Z., Seifert, P. and Ballauri, A., 2001. New and mature carbonate plays revive exploration in Albania. 

EAGE 63rd Conference & Technical Exhibition, Amsterdam, The Netherlands, 11-15 June 2001, P518. 

Frank, F. C. and Stroh, A. N., 1952. On the theory of kinking. Phys. Soc. Proc. Ser. B. 65:811-821 

Melo, V. et al., 1991/a. Tectonic windows of the Outer Zones in the eastern regions of Albanides. Bui. 

Shkenc. Gjeologjike, No. 1, pp. 21-29, Tirana (in Albanian). 

Melo, V. et al., 1991/b. Thrust structures in the Albanides. Bui Shkenc. Gjeologjike, No. 1, 7-20, (in 

Albanian). 

Van geet, M., Swennen, R., Durmishi, C, Roure, F. and Mushez Ph., 2001. Paragenesis of Cretaceous to 

Eocene carbonate reservoirs in the Ionian fold and thrust belt (Albania): relation between tectonism and 

fluid flow. 

49




INSTRUMENTAL SEISMOLOGICAL DATA and GEOLOGICAL INVESTIGATION 

of 2009 EARTHQUAKE, at GJORICA, DIBRA REGION 

E. DUSHI, Y. MUCEKU, J. SKRAMI & M. ZACAJ 

Institute of Geosciences, Polytechnics University of Tirana, Albania 

e.dushi@geo.edu.al; edmonddushi@yahoo.com 

(Poster presentation) 

On September 6, 2009 a strong earthquake (MW = 5.2), occurred in the northeastern Albania, 

in Gjorica, Dibra region, causing many damages in a large area and was felt till central part 

of Albania. The macroseismic effects have been revealed from field geological and 

seismotectonic observations. This earthquake has been followed by 678 aftershocks, where 

130 are localized. From earthquake analysis, the source parameters for this event and 13 

immediate subsequent aftershocks are determined. To perform this investigation through re 

evaluation of parameters, data recorded from BB seismic stations of Albanian Seismological 

Network have been used, (Fig. 1). 

Fig. 1: Registered BB wave forms of September 6, 2010 event (21:49 UTC) event, from BCI, PUK, 

PHP, TIR, KBN and SRN seismic station of Albanian Seismological Network. 

From the focal mechanism solution results that this earthquake has been triggered from the 

activation of oblique normal fault (Fig. 2), with an active plane striking 210 0 -219 0 NE, dipping 40 0 

and sliping -90 0 . This solution is in good acordance with the field geological observations. 

51

Fig. 2: Epicentral map of September 6, 2009 (21:49 UTC) main shock and its imediately subsequent 

aftershocks in connection with the distribution of BB seismological stations and focal mechanism 

solution of Gjorica earthquake. 

Spectral analyze has been performed based on the Brune (1970) theoritical model for source 

displacement spectrum, taking into acount various assumption on geometrical spreading factor and 

anelastic attenuation due to local heterogenity effect on traveling seismic wave energy (Fig. 3). 

Fig. 3: Displacement Spectras from horizontal components, for the September 6, 2009 event (21:49 

UTC). 

Seismic energy, radiated from September 6, 2009 event source express a significant macroscopic 

parameter to evaluate the seismic potential witch lead to the macroseismic effect in a broad area. To 

determine this parameter, dynamic methode has been used. This methode takes into acount the 

velocity power spectra integrated over frequency. These corrected velocity spectra for each of the 

horizontal component have been determined (Fig. 5), from velocity seismic traces corrected for the 

effect of recording instrument response, (Fig. 4). 

Velocity 

0.0001 

0.0000 

-0 .0 0 0 1 

0.0 0.5 1.0 1.5 2.0 2.5 3.0 

0.0001 

Z 

0.0000 

-0 .0 0 0 1 

0.0 0.5 1.0 1.5 2.0 2.5 3.0 

0.0001 

N 

0.0000 

-0 .0 0 0 1 

m /s 

0.0 0.5 1.0 1.5 2.0 2.5 3.0 

Time m in 

� 

Fig. 4: Three velocity trace waveforms, corrected for instrument response, of BCI records of 

September 6, 2009 event (21:49 UTC). 

52 

E

Fig. 5: Power Velocity and Cumulative Power Velocity Spectra from horizontal components, for the 

September 6, 2009 event (21:49 UTC). 

Achieved values from spectral analysis, for the main event are seismic moment M0 = 7.9 x 

10 23 dyne-cm, static stress drop �� = 54.8 bar and seismic energy ES = 2.3 x 10 19 erg, slightly 

different from respective previously ones. 

From point of view of the geological and tectonics-neotectonics phenomena the region where 

the studied zone is included take part in Krasta- sub-tectonic zone, which include in external 

area of Alpine folding. It is strongly affected by pre-Pliocene tectonics movement. As, it is 

seen in the Vlora-Elbasan-Diber fault as weak environment, where the evaporate has break 

through the sedimentary deposits of the Triassic-Eocene-Oligocene- rocks and erupted. All 

these bring proofs the evaporate deposit when are in motion process generate the earthquake. 

Fig 6: Geological map of studied region 

The seismic hazard at a place has a direct connection with the geology in the location. Areas with hard 

rock’s as limestones and ultrabassic deposits, have a lower seismic hazard than areas with soft rocksflysch 

and molasses and liquid sediments. The Dibra earthquake is concentrated on the north of the 

Okshtuni tectonic window and, in a zone which is referred to as the Okshtuni deep fault, a tectonic 

zone which starts at Vlora fault and continues to Elbasan and end up northeast of Dibra at the area of 

the Macedonia. One factor, which affects the attenuation of the seismic waves, is the geology (Fig. 6). 

Keywords: seismic moment, stress drop, radiated seismic energy, geological investigation 

53




IMPACT of BASEMENT CONFIGURATION and SEDIMENT ARCHITECTURE on 

GRAVITY GLIDING on UNDER-COMPACTED SHALE DECOLLEMENTS 

Nadine ELLOUZ-ZIMMERMANN*, Raymi CASTILLA*, François ROURE*, Khalid 

AL HOSANI**, Saleh AL MAHMOUDI** and Abdullah GAHNOOG ** 

*IFP Energies Nouvelles, 1-4 av de Bois-Préau, 92856 Rueil-Malmaison, France. 

** Ministry of Energy, Abu Dhabi, Emirates 

What are the dominant parameters which governed the tectonic style in gravity-driven 

complex tectonics on deep shale décollements levels along margins? One of the first order 

parameter concerns overloading process on platforms. Associated, either to intense 

erosion/deposition in compressive margins, or driven by rivers which convey huge amount of 

sediment up to deltas, the overloading in strongly link with the development of overpressure 

cells within deep shale layer. Location of the depocenters or of the prograding deltas through 

time, should also be a critical parameter for the evaluation of deformed traps. 

To be able to identify some criteria of the generation of deformed zones, the architecture of 

the deep structures was analyzed through time, via analogue models, in order to evaluate the 

impact of several parameters which could vary in 3D. All the models have been acquired with 

X-Ray tomography at IFP, and calibrated at a first order scale on subsurface data from 

Chamak Survey- in the Makran compressive margin, in the Sinu accretionary prism and in the 

East Oman Margin, atypical passive margin developed on the Oman Emirates Fold-and 

Thrust belt. 

Several sensitivity tests have been done on décollement level configuration; dip, interruption 

on basement blocks, and various ratio between ductile and brittle layers.. 

It appears that the characteristics of initial configurations either of the basement, or of the 

sedimentary patterns governed not only the distribution and the direction of the normal 

growth faults system, but also the location and the amplitude of the down-slope compressive 

deformation. 

Cylindrical progradations of various extension -above or behind the compressive front, can 

freeze the gravity-driven compressive front and evenly can be dissected by a new growth fault 

system, or reactivated and translated downslope. 

Out coming results allow 1) to improve seismic interpretation in blind areas when 

overpressured shale mobilization processes dominated 2) to estimate the timing and the 

nature of the deep structures development, and 3) to be predictive on the preservation of the 

deepest traps. 

55

Mary FORD 




CORINTH RIFTING and its ROLE in the GEODYNAMIC EVOLUTION 

of the AEGEAN-IONIAN REGION 

1 Nancy Université, CRPG, 15 Rue Notre Dame des Pauvres, B.P.20, 54501, Vandoeuvre-lès- 

Nancy Cedex, France 

The Gulf of Corinth (100 km by 30 km) is an active rift within a rapidly evolving diffuse plate 

boundary linking the dextral Kefalonia and North Anatolian faults. It lies above the NW 

subducting African plate. The rift initiated sometime in the late Pliocene and was 

superimposed on the NNW-SSE trending Hellenide orogenic belt of Oligocene age. The synrift 

stratigraphy and structure of the early Corinth rift is today uplifted and spectacularly 

exposed along the southern margin of the Gulf. Major normal faults are planar and dip 

predominantly north (45° to 65°) with an average strike of N110°. Kinematic analyses reveal 

a paleo-extension direction varying from N355° to N020°, sub-parallel to present day 

extension across the Gulf. Detailed mapping of syn--rift stratigraphy reveals three phases of 

rifting. Fault activity and syn-rift depo-centres migrated north with time as the rift narrowed. 

Total N-S extension across the whole western rift is estimated to be 11 km (7.2 km offshore 

and 3.8 km onshore). Extension accelerated significantly at around 1.4 Ma and at 800-600 ka 

when rapid uplift of the south flank started. Present day geodetically measured extension rates 

are 1.6 cm/a in the west and 1.1cm/a in the east. Crustal layering generated by the stacking of 

Hellenide thrust sheets has strongly influenced the dynamics of the rift and generated lateral 

variations in rift geometry. However crustal structure and rheology are so far poorly defined. 

This paper looks at the controversial and problematical role of the N-S Corinth rifting within 

the regional geodynamic evolution of the Aegean-Ionian area. 

57

Alfred FRASHERI 




TEMPERATURE SIGNALS FROM ALBANIDES DEPTH 

Faculty of Geology and Mining, Polytechnic University of Tirana 

In the paper are presented the result of the geothermal modeling in Albanid-1 and Albanid-2 lines. 

These modeling are part of geothermal studies in Albania during the 90 years, in the framework of 

Geothermal Atlas of the Albania, European Geothermal Atlas and European Geothermal Resources 

Energy Atlas. 

Geothermal gradient changes from western to the eastern part of the Albania, and in the depth, too. 

The gradient values vary from 15-21.3 mK/m in Pre-Adriatic Depression. According to the 

modeling results, deeper than 20 km is observed decreasing of the gradient. This change of the 

gradient is coincided with the top of the crystal basement. In the ophiolitic belt of the Inner 

Albanides, the geothermal gradient has a value up to 36 mK/m at northeaster and southeastern part 

of the Albania. Decreasing of the gradient are observed deeper than 12 000 meters in this side of 

Albania, at the top of the Triassic salts deposits. In the both lines are observed that the temperatures 

in ophiolitic belt are higher than in the sedimentary basin, at the same depth. 

In the Heat Flow Density Map of Albania, is possible to observed two particularities of the 

scattering of the thermal field of the Albanides: 

Firstly, 42 mW/m 2 is maximal value of the heat flow in the External Albanides. At the eastern part 

of Albania, the heat flow density values are up to 60 mW/m 2 . Radiogene heat generation of the 

ophiolites is very low. In these conditions, increasing of the heat flow in the ophiolitic belt, are 

linked with heat flow from the depth. According to the Alb-1 line, the granites of the crystal 

basement, which have the possibilities for the great radiogenic heat generation represents the heat 

source. In ophiolitic belt, is observed decreasing of the MOHO discontinuity depth. 

Secondly, in the ophiolitic belt are observed some hearth of higher heat flow density. Heat flow 

anomalies are conditioned by intensive heat transmitting through deep and transversal fractures. 

These fractures are conditioned location of the geothermal energy sources. According to the 

calculation of different geothermometers, the aquifer estimated temperatures are 144 to 270 o C. 

Based on the geothermal modeling, one can suppose that thermal waters rises from 8-12 km deep, 

where temperature attains to 220 o C. 

59




GEOPHYSICAL OUTLOOK on STRUCTURE of the ALBANIDES 

Alfred FRASHERI 1 , Salvatore BUSHATI 2 , Vilson BARE 3 

1 Polytechnic University of Tirana, Faculty of Geology and Mining, Tirana, Albania. 

2 Academy of Sciences of Republic of Albania, Tirana, Albania 

The Albanides represents the assemblage of the geological structures in the territory of Albania. 

This paper presents the structural analysis of the Albanides according to the seismological, 

reflection seismic, gravity, magnetic, electrical, and geothermal surveys. Two major 

peleogeographic domains form the Albanides. The Internal Albanides formed part of the 

Subpelagonian Trough. The External Albanides was developed out of the western passive margin 

and continental shelf of the Adriatic plate. Regional gravity anomalies and seismological data are 

interpreted as caused by the variation of the depth of Moho discontinuity, and a block construction 

of the crust. The Earth crust in Albanides is interrupted by a system of longitudinal fractures in NW 

- SE direction and transversal fractures. Intensive Bouguer anomalies and turbulent magnetic field 

with weak anomalies characterize ophiolitic belt of the Internal Albanides. These data show about 

the allochton character of ophiolites. The relations between the Internal and the External Albanides 

have a nape character, going toward SW. A joint characteristic of structural belt of Ionian and Kruja 

zones in External Albanides is their westward thrusting, too. Two tectonic styles are observed in the 

Ionian tectonic zone: duplex and imbricate tectonic. Miocene and Pliocene molasses of Peri- 

Adriatic Depression cover Western part of Ionian zone. 

Interpretation of the results of integrated geophysical surveys, in the framework of geological 

studies is presented in the paper. 

61

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41.5° 

41° 

40.5° 

40° 

0 50 km 

42° 

41° 

40° 

Durres 

Karavatsas 

Lagoon 

C.p. 

Nartës 

Lagoon 

Tirana 

Ionian 

Sea 

Erzen 

Vlorë 

19° 20° 21° 

S hkumbin 

Ap.A. 

Ar.A. 

Seman 

Tirane 

S.A. 

Tepelenë 

Reverse Fault 

Normal Fault 

39.5° 

19° 20° 

? 

? 

Lushnje 

L.T.T. 

Elbasan 

Berat 

E.G. 

Pa.D. 

T.T. 

O 

s u m 

V j o s a 

Sarandë 

Librazdhi 

Gramsh 

Strike-slip Fault 

Anticline Fold 

Progradec 

Devo l Vithkuq 

W.E.N.F.S. 

Ersekë 

Permët 

K.N.F.S. 

Aristi 

Ioannina 

Borders 

Ohrid 

Lake 

N.N.F. N.N.F. 

W.G.N.F.S. 

N.N.F. 

N 

Prespa 

Lake 

Korçë 

Konitsa 

P.W.N.F. 

K.N.F. 

Kipi 

Scale 

0 20km 

Figure 1. Neo-tectonic map of the Southern Albania and North-western Greece (Modified from Aliaj et al., 1996 and Carcaillet, et 

al, 2009). Areas located within 200 m above Sea level are in light grey. Dark grey stars indicate published data (Lewin et al., 1991; 

Hamlin et al., 2000; Woodward et al., 2001; Carcaillet et al., 2009) and red stars indicate data computed in the present study. Fault 

and fold types are described in the picture caption and the overall current tectonic deformation is represented by black arrows (from 

Jouanne et al., submitted). (C.p.) Coastal pop-up; (Ar.A.) Ardenica Anticline; (Ap.A.) Apollonia Anticline; (S.A.) Shkumbin 

Anticline; (T.T.) Tomorrica Thrust; (L.T.T.) Lushnje - Tepelenë Thrust; (B.N.F.) Bulcar Normal Fault; (E.G.) Elbasan Graben; 

(N.N.F.) Nerotrivi Normal Fault; (K.N.F.S.) Konitsa Normal Fault Systems; (P.W.N.F.) Papingo West Normal Fault; (K.N.F.) Kipi 

Normal Fault; (W.G.N.F.S.) West Graben Normal Fault Systems; (W.E.N.F.S.) West Ersekë Normal Fault Systems; (PaD) 

PaleoDevoll. 

well as from in situ produced 10 Be and radiocarbon ( 14 C) dating specifically performed for this 

study. We dated organic residues (eleven 14 C ages) and quartz rich pebbles collected into layers 

64 

21°

Incision rate (m/ka) 

developed during the ultimate flooding event and considered the value as the age of abandonment 

of the alluvial terrace. This implies that the age of the terrace abandonment is contemporaneous to 

the age of deposition of the highest terrace layer. Cosmonuclide (in situ produced 10 Be) age 

determinations are in process on siliceous rich pebbles collected along depth-profiles of two 

terraces of the lower Skhumbin and on the top of the upper Osum. Incision rate has been calculated 

by dividing the elevation of the terraces above the river by the age of the upper surface of the 

terraces; the vertical motions of the faults have been deduced from the local change of the incision 

rates. 

Results and discussion 

The results are shown in the three following diagrams (Fig. 2, 3, 4) that allow comparing the 

incision rate, the location of the faults and the aspect of the river profile for the three rivers (The 

lower Shkumbin is considered as the paleo-lower part of the Devoll). A table (Table 1) indicates the 

most active structures evidenced by a step. 

West 

5 

4.5 

Post LGM 

Pre LGM 

East 

4 Linear regression Post LGM 

3.5 

by tectonic blocks 

3 

2.5 

2 

1.5 

1 

0.5 

0 

W.E.N.F.S. 

120 145 170 195 220 

Distance from the Sea (km) 

Figure 3. Evolution of the incision rate along the river 

profile of the Vjosa. bed. In the river profile are located the 

Lushnje - Tepelenë Thrust (L.T.T.), Nerotrivi Normal fault 

(N.N.F.), Konitsa Normal Fault Systems (K.N.F.S.) 

Papingo West Normal Fault (P.W.N.F.). 


2.0 

1.6 

1.2 

0.8 

0.4 

0 

West 

Pre LGM 

Linear regression Pre LGM 

by tectonic blocks 

23 m 

0.9 m/ka 

L.T.T. 

T.T. 

5m 

0.2 m/ka 

S.A. 

28.6 m 

1.7 m/ka 

E.G. 

2.1 m/ka 

35 m 

11 m 

0.4 m/ka 

1000 

500 

0 

Elevation above 

Sea level (m) 

Figure 2. Evolution of the incision rate along the 

river profile of the Osum. Left axis is the calculated 

incision rate; right axis is the elevation of the presentday 

river bed. Colour of the diamonds refers to the 

different terraces units. Into the lower box, appear the 

actual river profile where are located the actives 

faults. Bold lines represent normal faults belong of 

West Ersekë Normal Fault Systems (W.E.N.F.S.) 

producing surface displacements and the dashed lines 

represent the Tomorrica Thrust (T.T.) which would 

not influence in the evolution of the river profile. 

60 85 110 135 160 185 

East 

T.T. B.N.F. W.G.N.F.S. 

25 50 75 100 125 150 175 

9m 

0.3 m/ka 

Elbasan Basin Korça Basin 

>1 m/ka 

Lower Shkumbin PaleoDevoll Devoll 


West 

1.2 

Figure 4. Evolution of the incision rate along the combined river profile of the lower Shkumbin and Devoll. In the river profile are 

located the Lushnje - Tepelenë Thrust (L.T.T.), the Shkumbin Anticline (S.A.), Tomorrica Thrust (T.T.), the Burcal Normal Fault 

(B.N.F.) and the West Graben Normal Fault Systems (W.G.N.F.S.) producing surface displacements. 

65 

1 

0.8 

0.6 

0.4 

0.2 

0 

Post LGM 

Pre LGM 

? 

3m 

0.2 m/ka 

? 

L.T.T. 

>0.8m/ka 

Konitsa Basin 

>0.4m/ka 

K.N.F.S. 

N.N.F. P.W.N.F. 

800 

400 

0 


Sea level (m) 

East 

1000 

500 

0 


Sea level (m)

Results suggest that: a) The incision rate reaches the greatest values in the Osum area; b) The 

incision is more strongly controlled by the normal faults than the thrust faults; c) The normal 

faulting linked to the East Albanian graben systems seems more active than the normal faulting that 

affects the North West part of Greece. 

Table 1. Kinematic of active structures active analyzed from the incision of the terraces levels of the Vjosa, Osum, 

Devoll and Shkumbin rivers. 

Name Structure River Vertical slip movement (m/ka) 

Coastal pop - up PaleoSeman ~ 0.1 ( Fouache et al, 2010) 

Shkumbin Anticline Shkumbin ~ 0.2 

Elbasan Graben Shkumbin > 1 

Lushnje - Tepelenë Thrust Shkumbin ~ 0.9 

Lushnje - Tepelenë Thrust Vjosa ~ 0.2 

Tomorrica Thrust Devoll ~ 0.4 

Burcal Normal Fault Devoll ~ 0.3 

Nerotrivi Normal Fault Vjosa > 0.4 

Konitsa Normal Fault Systems Vjosa > 0.4 

Papingo West Normal Fault Vjosa ~1.8 between 25 and 17 Ka (Carcaillet, et al, 2009) 

West Graben Normal Fault Systems Devoll > 0.8 

West Ersekë Normal Fault Systems Osum 1.7 – 2.1 

References 

Aliaj, Sh., Melo, V., Hyseni, A., Skrami, J., Mëhillka, Ll. Muço, B., Sulstarova, E., Prifti, K., Pashko, P., Prillo, S., 1996. 

Neo-tectonic map of Albania, scale 1: 200000. Archive of seismology Institute, Tirana, Albania. 

Aliaj, S.H., 1997. Alpine geological evolution of Albania. Albanian Journal of Natural and Technology Sciences 3, 69-81. 

Aubouin, J, Ndojaj, I., 1964. Regard sur la géologie de l’Albanie et sa place dans la géologie des Dinarides. Bulletin de la 

Société Géologique de France 6, 539-625. 

Baker, C., Hatzfeld, D., Lyon-Caen, H., Papadimitriou, E., Rigo, A., 1997. Earthquake mechanisms of the Adriatic Sea 

and Western Greece: implications for the oceanic subduction-continental collision transition. Geophysical Journal 

International 131, 559-594. 

Carcaillet, J., Mugnier, J.L., Koçi, R., Jouanne, F., 2009. Uplift and active tectonics of southern Albania inferred from 

incision of alluvial terraces. Quaternary Research 71, 465-476. 

Fouache E., Vella C., Dimo, L., Gruda, G., Mugnier, J-L., Denèfle, M., Monnier, O., Hotyat, M., Huth. E., 2010. 

Shoreline reconstruction since the Middle Holocene in the vicinity of the ancient city of Apollonia (Albania, Seman and 

Vjosa deltas). Quaternary International 216, 118–128 

Goldsworthy, M., Jackson, J., Haines, J., 2002. The continuity of active fault systems in Greece. Geophysical Journal 

International 148(3), 596-618. 

Hamlin, R.,Woodward, J., Black, S., Macklin, M.G., 2000. Sediment fingerprinting as 580 a tool for interpreting long- 

term river activity: the Voidomatis basin, NWGreece. In: 581 Foster, I.D.L. (Ed.), Tracers in Geomorphology. Wiley, 

Chichester, 473–501. 

Jouanne, F., Bushati, S., Mugnier, J.L., Shinko, I., Pasha, M., Koci, R. GPS constrains on current tectonics of Albania. 

Geophysical Research Letters, Submitted. 

Koçi, R., Bushati, S., Mugnier, J-L., Perenjesi, E., 2009. The river tarraces-indicators of the neotectonic movements in 

Albania. 5 th Congress of Balkan Geophysical Society. Belgrade, Serbia. 

Lewin, J., Macklin, M.G., Woodward, J.C., 1991. Late Quaternary fluvial sedimentation in the Voidomatis basin, Epirus, 

Northwest Greece. Quaternary Research 35, 103-115. 

Macklin, M.G., 2000. Sediment fingerprinting as a tool for interpreting long-term river activity: the Voidomatis basin, 

NW Greece. In: Foster I.D.L. (Ed.), Tracers in geomorphology. Wiley, Chichester, pp. 473-501. 

Roure, F., Nazaj, S., Mushka, K., Fili, I., Cadet, J.P., Bonneau, M., 2004. Kinematic evolution and petroleum systems - 

An appraisal of the Outer Albanides. In: Mc Clay K.R. (Ed.), Thrust tectonics and hydrocarbon systems. AAPG memoir 

82, pp. 474-493. 

Woodward, J.C. Hamlin, R.B.H., Macklin, M.G., Karkanas, P., Kotjabopoulou E., 2001. Quantitative sourcing of 

slackwater deposits at Boila rockshelter: A record of late-glacial flooding and palaeolithic settlement in the Pindus 

Mountains, Northern Greece. Geoarchaeology 16(5), 501-536. 

66




CONTRACTION and VERTICAL MOVEMENTS in the GARGANO PROMONTORY 

and ADJACENT OFFSHORE: IMPLICATION for the TECTONICS of the SOUTH 

ADRIATIC DOMAIN 

Nicolaas J. HARDEBOL and Giovanni BERTOTTI 

Delft Univ. of Techn., Stevinweg 1, 2628 CN Delft, the Netherlands; VU University, De 

Boelelaan 1085, 1081 HV Amsterdam, The Netherlands; T +31 15 27 81352; E 

N.J.Hardebol@tudelft.nl 

Introduction 

The Adriatic plate has been described as a double-verging plate that is bordered to the west by 

the Apenninic and to the east by the Dinaric-Helvetic fold-and-thrust belts (Figure 1a). The 

interior of the plate supposedly hosts a north-south trending flexural bulge from Istria to the 

Gargano promontory (and the Apulian Ridge), which divides the Adriatic basins in respect to 

their relative foreland position to either the Apenninic or Dinaride orogenic systems. The 

Neogene deformation history and vertical motions in the interior of the Adriatic plate is 

subject to flexural forcing or compressional effects transmitted from the plate margins. This 

study present new field and offshore seismic data from the Gargano Promontory and adjacent 

Southern Adriatic Basin to examine their deformation history. 

The Southern Adriatic Basin (SAB) stretches southeast-ward offshore of the Gargano and 

Puglia coastlines (Figure 1a) and is underlain by a basement of Triassic-Lias salts to platform 

carbonates and a Lias-Cretaceous succession of mostly pelagic carbonates and marls that 

show an eastward, Dinaric-Hellenic facing dip. The SAB contains an Oligocene to Quaternary 

succession of mainly siliciclastics and calcarenites and subject to tilting and faulting of strata 

that are commonly regarded as transtensional and transpressional expressions linked to 

basement lineaments. 

The Gargano Promontory (GP) to the north forms up to 1000m relief and comprises mostly 

Jurassic-Cretaceous carbonates. The GP exhibits a peculiar morphological shape with four 

prominent peneplains that are divided by high and steep slopes (Figure 1d). Miocene shallowwater 

limestones cover the eroded substratum unconformably and are found over most of the 

Gargano Promotory. Post-Lower Messinian deposits however are scarce and especially 

developed onto the two lowermost peneplains at 80m and 200m along the southern border of 

the GP (Figure 1b). These Mio-Pliocene deposits cover erosional surfaces and contain 

diagnostic coastal cliff facies linked to abrasive marine terrace that help deciphering the 

Tertiary deformation and relief development (Casolari et al., 2000; Bertotti et al., 2001). 

This study presents new data from the GP and from offshore seismic profiles of the SAB. We 

examine their contrasting physiographic expression in effect to a Miocene-Pliocene 

contractional and uplift-subsidence history. We especially focus on the marine terrace 

sediments in association to their tilted substratum for the GP and on the coeval depositional 

and deformation history in the adjacent SAB. The onshore field data and offshore seismic 

interpretations are combined aiming at a more univocal picture of the kinematics and vertical 

motions for Tertiary times. 

67

Uplift of the Gargano Promontory as recorded by abrasion terraces 

Rightly positioned on the presumed axis of the double-plunging Adriatic plate, the high relief 

of the Gargano Promontory (GP) appears as the most exquisite forebulge expression. 

However, despite this commonly held interpretation as flexural bulge, relief and structures of 

the GP pose certain challenges to this bulge concept. 

New field data has been acquired to examine the geometric affinity between the peneplains, 

the overlying deposits and relationship to structures from the Jurassic-Cretaceous substratum. 

Casolari et al. (2000) provided the sedimentological framework for the sediments that overly 

some of the peneplains by emphasising their distinct marine signature. Two marine 

formations are distinguished on the two lowermost terraces and which classify the erosional 

surfaces as marine terraces: the Rignano formation on a 200m terrace level and the Gravina 

Calcarenites formation (middle-upper Pliocene) on a 80m terrace level (Casolari et al., 2000). 

Our field observations show that the scarcely distributed deposits are remnants of a proximal 

coastal setting deposited on top of an abrasive marine terrace adjacent to coastal cliffs. 

Gravity derived coarse breccias are found in direct affinity with these cliff-walls, while finer 

breccias and conglomerates are found in the more distal parts of the terraces and contain a 

more marine calcarenite matrix. Distinct marine indicators are mainly found in the distal 

biocalcarenites in which some marine fossil assemblages have been previously identified and 

described by Casolari (2000). A marine fingerprint is much more difficult to find for the 

conglomerates and breccias in direct contact with the cliff-wall. Alternative indicator for the 

marine origin is the erosional contact itself with the sharp and flat surface between the 

calcarenites truncating tilted substratum rocks and especially the occurrence of some wellpreserved 

wave-cut notches in the cliff-walls (Figure 1e). 

The Mass a Palacane location (MAP; see Figure 1c) on the 200m terrace contains the 

complete coastal facies with breccias and conglomerates juxtaposed to a sub-vertical cliffwall 

and grading southward over a distance of 300-400m into more distal calcaranites. Coarse 

breccias with clasts of 30-40 cm floating in a red dusty matrix are found in a small fringe at 

the steep slope and change laterally rapidly into widespread conglomerate and pebble-rich 

calcarenite. The clasts have a monomictic composition similar to the Jurassic-Cretaceous 

series of the terrace substratum and cliff walls. 

The two locations positioned on the lower 80m terrace, at base of the slope connected with the 

200m terrace level, are the Posta Mapuzza (POM; Figure 1c) in the east and the Masseria 

Figure 1. (a) Overview map of the Adriatic plate and location of the studied areas, (b) Structural map of the 

Gargano Promontory, (c) Field locations at the 80m and 200m terraces, (d) Geomorphological panorama and 

(e) Mass a Palacane location (MAP) with field observations of a coastal cliff and wave-cut notch.




KINK BANDS and CHEVRON FOLDS CHARACTERISTICS of the SARANDA ANTICLINE: 

ESTIMATION of the "GEOLOGIST's MOSAIC", SOUTH-WESTERN ALBANIA 

Prof. Dr. Çerçis DURMISHI, Polytechnic of Tirana, Albania, cecodurmishi@yahoo.com 

Prof. Vangjel MELO, Polytechnic of Tirana, Albania 

Ing. Ervin LULA, Island International Exploration BV-Albania. elula@islandoilandgas.com 

Observations of events leading to development of kink bands, their origin, and changes in their 

morphology are recorded during the deformation in the "Geologist's mosaic" 1 ' in southern Albania. 

Kinking in natural deformed limestone strata has been investigated to determinate the complete history, 

of this deformation during the Paleocene. A model is presented to show in general terms the 

characteristics of these types of folds and also to explain the origin of observed kink. 

Key words: Tectonic, Kink Bands, Chevron Folds, dome-brachianticline, Ionian Zone, Paleocene, 

clay-siliceous-carbonate beds 

"GEOLOGIST'S MOSAIC" 

The purpose of this poster is to qualitatively and quantitatively analyse an outcrop with kink bands in southern 

Albania (nearby the city of Saranda), to place this particular deformation feature into its local and regional 

context, to discuss the structural and tectonic significance of kinking and to explain the tectonic conditions in 

which kinking occurs in the study area. 

In the geological interpretation and aspect this "MOSAIC" represents a complication dome-brachianticline in the 

western flank of the Saranda anticline. This section viewed as an asymmetric anticline. The south-eastern flank 

has a gentle dipping (about 25° - 30°), while the north-western flank has steepness bigger then that, almost 

vertical (Fig. 1). 

In terms of geological setting this section is of Paleocene in age. Mostly, the centre of the structure is covered 

as a "roof from a thick turbidite horizon, which uncovered in the south-western flank of the mosaic. The 

carbonate strata are represented from thin-bedded limestones with reddish and/or greenish cherty intercalations 

few centimetres thick and from very thin clay-siliceous-carbonate beds. 

The difference in thickness between turbidite limestone strata which have been repeated in the section and 

which has a thickness of 1 - 2 meters (competent layer), and thin limestone layer of about 0.4 meters 

(incompetent) strata with cherty intercalations which are also dominant in the section, have been created a 

kink bands and chevron folds mosaic inside this section with different shapes, and with a moderate ratio "n" (n 

= d2/di, di = competent layer; d2 = incompetent layer). The estimation of the shortening for the whole structure, 

caused by the "megakinks" is between 33% and 36%. These kink bands and chevron folds are not characteristic 

for the turbidite limestone strata, which has been as boundaries inside of which have been developed the 

disharmonic microfolds. 

Geometric characteristic of the microfolds are very different, they change in the south-eastern flank of the 

mosaic, in the core, north-western flank as if from the top to the bottom of the mosaic. 

The south-eastern flank of the mosaic is less affected from the kink bands. This flank, which has a gentle 

dipping and could have been affected by the tectonic press or even extension, that caused non-development of 

the typical microfolds but just some flexural slips and some kink bands. If it will supposed that both of the 

turbidite horizons where thin carbonate strata it's attached, will move up and down, the stress create a 

orientation when the shear stress acted as a band and create the kink bands. 

69

features with a NE-SW shortening direction. This structural interpretation can be further 

depicted from Figures 2b-c that show our interpretations of the Gondola and Grazia structures 

in the D438 and D452 profiles, respectively. The Gondola Ridge has been previously 

interpreted as a horst-like feature bordered to the north by a normal fault and with the SAB 

northern section as the down-faulted hanging wall (Alteriis and Aiello, 1993). Instead, we 

consider that the tilting and uplift of the Mesozoic basement and the Miocene-Pliocene cover 

are best explained by thrusting propagated along a decollement level at the Upper Triassic 

Burano salt layer. The Gondola Ridge in the western part of the SAB contains an elevated 

Mesozoic succession covered by only 300m thin Pliocene-Quaternary veneer, as documented 

by the Gondola Well located at the crest of the Ridge. 

Truncation of tilted isopach reflectors of Miocene strata by the Pliocene-Quaternary 

succession suggests that uplift of the Gondola Ridge and rotation of its southern flank must 

have occurred in the latest Miocene-earliest Pliocene time. 

Synthesis and conclusions 

Recognition of two distinct marine cliff facies at the escarpments upward from the 80m and 

200m terraces make clear these peneplains were formed successively by marine abrasion. No 

evidence is found that the vertical slopes dividing the peneplains are normal fault 

escarpments. These field observations from the southern flank of the Gargano Promontory in 

conjunction with earlier work (Bertotti et al., 1999) oppose the commonly held perception of 

the GP as a flexural bulge. A bulge may display normal faulting from flexural fibre stresses, 

although such faulting would be expected to be subordinate to presumed large-wavelength 

antiformal tilting of the bedding. However, the escarpment that climbs from the 200m 

peneplain lacks such fault traces and instead a marine-erosive origin is evidenced with welldeveloped 

marine cliff-facies. Moreover, much short-wavelength west verging folding 

suggest substantial shortening with tilting best explained by fault-bend folding of (blind) west 

verging thrusting. 

Both the structural style and timing of vertical motions correlate well with the new 

interpretations from the offshore SAB seismic lines. Pliocene-Quaternary strata overly 

strongly tilted Mesozoic to Miocene rocks that were subject to Middle-Late Miocene 

contraction, resulting in several hundreds of meters of relative uplift. Also in the southern 

Gargano uplift and tilting of the substratum occurred by fault related folding due to NE-SW 

contraction during the middle Miocene to pre-Messinian time. This contrasts with earlier 

interpretations of Pleistocene uplift and/or a NE-SW tensional origin. Such an interpretation 

poses interesting kinematic problems with the adjacent Southern Adriatic Basin when their 

main structures are interpreted in the context of transtensional tectonics and without any 

major contractional structures reported for the SAB (Bertotti et al., 1999). Instead, with a 

reinterpretation of the Gondola Ridge, as dominant compressional feature in the SAB, a less 

isolated and regionally and kinematically much more univocal picture becomes apparent. 

References 

Alteriis, G., Aiello, G., 1993. Stratigraphy and tectonics offshore of Puglia (Italy, southern 

Adriatic Sea. Marine Geology 113: 233-253. 

Alteriis, G., 1995. Different foreland basins in Italy: examples from the central and southern 

Adriatic Sea. Tectonophysics 252: 349-373. 

Bertotti, G., Casolari, E. and Picotti, V., 1999. The Gargano Promontory: a Neogene 

contractional belt within the Adriatic plate. Terra Nova 11: 168-173. 

Casolari, E., Negri, A., Picotti, V. And Bertotti, G., 2000. Neogene Stratigraphy and 

Sedimentology of the Gargano Promontory (Southern Italy). Eclogae geol. Helv. 93: 3-23. 

70




STRATIGRAPHY and LITHOLOGICAL COMPOSITION of the QUATERNARY 

SEDIMENTS in ALBANIA 

Jakup HOXHAJ, Fatbardha CARA 

Instituti i Gjeoshkencave, Universiteti Politeknik i Tiranës 

Hasan KULIÇI 

Shërbimi Gjeologjik Shqiptar 

Shehribane ABAZI 

Komsioni i Pavarur i Minierave dhe Mineraleve Kosove 

Contact: jakuph2001@yahoo.com 

Stratigraphy and lithofacial content of Quaternary deposits, along, the Albanide geological 

structure from the choice and from the very wide spread, is a very individual important in the 

context of the overall geological study. Thanks to these studies, especially those after 90të years, 

these deposits, are now more determined, in lithology, in genesis and in their age. The new 

deposits are Plio- Quaternary and Quaternary with clear stratigraphic position, which fill all near 

the Adriatic low land interior, potholes and slopes of the end of their, glacial and the karstic 

relieve, also glacial lake depressions. In general, these are product of erosive are accumulative 

transformations of glacial activity, the water network as a whole, incline of the slopes, 

anthropogenic activity, so climate transformations in the territories with slowly neotectonic 

activity. 

In the determination of their age, for the specifics they have besides the classical methods and 

relativity, are applied the new and specific methods of the different types, according to the 

modern experiences. 

The global tectonic lead to investigation relate to the favorable zones for the forming of a 

sedimentary basement, also the ways about its evolution. 

There are differenced 5 main levels of the terraces with relative elevation respectively: 10-20m, 

30-45m, 60-80 m, 90-100 m and 120-130 m, which have the development and are saved well in 

the middle flows of the rivers, especially in the right side of them. This is explained, as the 

general factors (planetary), also with local factors as are: the different intensity of the tectonic 

movements owing to the different order of the geological structures and the no same 

development of the water net in two sides of the valley. 

The river terraces, are consider of the tectonic and climatic character, where during a climatic 

cycle (glacier, interglacial), is formed a river terrace. The forming of the river terraces is made, 

mainly during the glacial periods, while, the forming of cones of the output (alluvions) which are 

superposed everywhere on terraces, must to be done in the end of these epochs, in the fazes of 

the glacier rapid melting. In this time must to be formed and the barriers, whose footprints there 

are, almost in all levels. The section of the terraces (their stairs) must to be done during the 

71

interglacial epochs, on which the rivers must to have had big amount of the water and so, must to 

be grown the their abrasive power. 

It is clear, that in this forming have influenced and the presence of the elevator movements. 

According to mainly, geomorphologic character we have: today Quaternary depositions (where 

are included the bed depositions, the gritty earth of the rivers and today alluvial fields), the upper 

Pleistocene depositions (the deposition of the firs terrace level), the middle Pliocene depositions 

(the depositions which construct the second level of the terraces), the deposition of the lower 

Pliocene (deposition which construct the second and third level of the terraces), the Plio- 

Pleistocene depositions (river and lake facies). 

The age division, are supported in the fact of the paleogeographic development, after three main 

sedimentary fazes: the lake faze (lower-middle and partly upper Pleistocene), the river faze 

(lower-middle-upper Pleistocene included and Holocene). The fact of the river depositions 

placement (terraces) up to deposition of the lake-river facies less deformed from the Vallahe 

folding. 

The strong turns as like as elbow in southern-western direction what the Devolli river gets in 

Gostima of Elbasan and Vjosa river in Kelcyra, happen from the presence of a lake in Elbasani– 

Cerrik region, in Quaternary period, with the elongate as a tongue in Mollas- Selite direction. 

So the Devolli River, during Quaternary is poured in this lake and only in the end of Pleistocene 

or in the beginning of the Holocene has got the turn to southwest, while the Kelcyra neckband is 

formed in a antecedence, so, the Vjosa River, during Quaternary has crossed in the way, in today 

direction. 

After geo-geomopholocical features, the walleyes of the Albanian rivers have favorable 

conditions for the constructing of the hydropower works, also after these conditions and results 

from complex works, has the premise for the placers. 

The alluvial depositions, almost the all kinds, have waterbearing capacity, with very importance 

for the water-drinking industry. 

72




SUBSALT DEPTH SEISMIC IMAGERY and STRUCTURAL INTERPRETATION in 

the DUMRE AREA, ALBANIE 

Anne JARDIN*, Luan NIKOLLA** and François ROURE* 

*IFP Energies Nouvelles, Rueil-Malmaison, France 

**National Agency, Albania 

Anne.Jardin@ifpenergiesnouvelles.fr 

The challenge of seismic exploration in fold and thrust belt setting is to optimize the depth 

seismic images of the deep structural objectives underneath complex overburden that may 

show strong horizontal and vertical velocity variations. In such areas, the seismic image is 

frequently of poor quality and the depth evaluation of deep layers is often false due to the 

perturbed propagation of seismic energy through the deforming lens of the overlying layers. A 

range of seismic processing tools, including post-stack and pre-stack depth migrations, are 

appropriate to estimate the accurate geometry of deep target structures and to improve the 

building of a depth structural model in this context. 

A strong combination of geological reasoning and depth seismic imaging processing can 

improve the understanding of the deep geological structures by reducing the uncertainties in 

depth geometrical and velocity model estimation. We propose an interpretative and iterative 

approach to the post stack depth migration method to guide the interpreter in the elaboration 

of a reliable subsurface model. 

We have applied this approach during an exploration study in the Dumre area, located in the 

Ionian Basin (Albania) which is a complex fold and thrust belt. The main objectives of this 

study were to understand the failure of a former exploration well and to propose a new 

location for the potential closure of the carbonate structure. This subsalt imaging study aims at 

illustrating the improvements obtained by application of this integrated seismic imaging 

method especially in the evaluation of a subthrust prospect in a tectonically complex belt 

setting. 

73




GPS CONSTRAINS on CUURENT TECTONICS of ALBANIA 

François JOUANNE (1), Jen-Louis MUGNIER (1), Rexhep KOCI (3), S. BUSHATI 

(2) , K. MATEV (1, 5), N. KUKA (3), I. SHIVIKO (3), M. PASHA (4), S KOCIU (6) 

(1) LGCA UMR CNRS 5025, Université de Savoie 

(2) Academy of Sciences of Albania 

(3) Institute of Geosciences of the polytechnical University of Tirana, Albania 

(4) Military Geographical Institute of Albania 

(5) Laboratory of Geodesy, Academy of Sciences of Bulgaria. 

(6) Professor on leave from Institute of Seismology of the Academy of Sciences of 

Albania, now 4631 N Lowell Avenue #E2, Chicago, Il 60630, U.S.A 

Current tectonics of Albania is documented by neotectonics indices and by a large 

number of medium size earthquakes. Focal mechanisms suggest the existence of current 

shortening across the external Albanides whereas internal Albanides are affected by E-W 

to N-S extension. To investigate the kinematics of Albanides, we integrate continuous 

and episodic GPS measurements with focal mechanisms of the Regional Centroid 

Moment Tensor catalogue. This study has allowed distinguishing a western Albania 

affected by westward motions relative to Apulia microplate, illustrating the ongoing 

collision of external Albanides, whereas inner Albanides present southward motion, 

increasing from north to south, relative to both Apulia and stable Eurasia. Active thrusts 

and backthrusts of external Albanides are segmented by strike-slip faults, the Llogara 

pass fault between the external Albanides and the Ionian zone appears to be particularly 

active (5mm/year). The Shkoder-Peja Fault Zone, between Dinarides and Albanides, is 

identified as the probable northern limit of an area including Albania and western Greece, 

affected by a clockwise rotation relative to Apulia and also the northern limit of the 

Balkan (inner Albanides, Macedonia, Bulgaria) affected by southward motion relative to 

Apulia and stable Eurasia. The other transverse fault zone, the Diber-Elbasani fault, 

appears to be mainly affected by a moderate extension. Compilation of published GPS 

data with our data set allow to identify the external-inner Albanides limit as the western 

border of the domain (inner Albania, northern Greece, Macedonia, Bulgaria) affected by 

southward displacements relative to stable Eurasia, whereas Shkoder-Peja fault form 

probably its northern limit. 

75




SEISMIC SEQUENCES in DIBRA REGION (ALBANIA) 


IMPLICATIONS for the SEISMIC HAZARD of the REGION 

Anastasia A. KIRATZI 

Department of Geophysics, Aristotle University of Thessaloniki, 54124, 

Thessaloniki, Greece (email: kiratzi@geo.auth.gr) 

The Albanian orogen belt, a segment of the Dinarides-Hellenides orogen, trends NNW- 

SSE and was developed by Alpine orogen processes related to the Apulia and Eurasia 

convergence and the closure of the Mesozoic Tethyan Ocean. The Dibra region, 

located in the eastern section of the Albanian orogen, near the borders with Fyrom, has 

been the location of intense seismic activity in recent instrumental times. A strong 

earthquake occurred on 30 November 1967 (GMT 07:23:50; Mw6.2; 41.41 ° N 20.44 ° E; 

h=9 km), which caused 19 deaths, 214 injuries and was associated with a N40 o E ~10 

km discontinuous or eroded surface rupture and 50 cm of vertical displacement. More 

recently, on 6 September 2009 (GMT 21:49) a moderate Mw5.4 earthquake sequence 

burst with its mainshock located ~6 km north of the 1967 epicenter at a distance of ~55 

km ENE from Tirana and ~25 km south of Peshkopie. This sequence was rich in 

aftershocks, the strongest of which occurred on 12 September 2009 Mw4.1 

(GMT18:42). The strongest events of the sequence were adequately recorded by the 

regional seismological networks of Albania, Greece and Fyrom. The neotectonic faults 

in the broader region are high-angle normal faults that have variable trends, N-S or 

NNE-SSW or NNW-SSE as this is manifested both in the earthquake focal 

mechanisms (Fig. 1) and the geomorphology. 

Here we study the 2009 sequence using broad band waveforms recorded by the 

Hellenic Unified Seismic Network (HUSN), which receives real-time waveforms from 

the neighbouring networks, to compute focal mechanisms, obtain the slip model and 

derive the shakeMap of the mainshock. The focal mechanisms of 18 of the stronger 

events of the sequence, obtained through time-domain moment tensor inversion, 

indicate that deformation is taken up by NNE-SSW trending normal faulting, in 

Kiratzi (2010). ILP Conference-Albania 

77

agreement with the ~E-W extension previously identified within the Albanian orogen. 

Our results show that the 2009 mainshock ruptured a roughly 9 km normal fault at a 

depth of 6km, which strikes ~N194 ° E and dips with an angle of ~45 ° to the west. The 

slip of the mainshock was confined in a single patch of ~9 km × 6 km, the average slip 

was 5 cm and the peak slip was 18 cm. 


Figure 1: Fault plane 

solutions for earthquakes 

with Mw>5.0 in Albania 

and neighbouring 

countries together with 

the 2009 Dibra events 

studied here. Note the 

nearly N-S trending faults 

(beach-balls depicted with 

light green) along the 

Albania orogen that take 

up deformation by nearly 

E-W extension. 

The slip model was incorporated in a forward modelling scheme to simulate the ground 

motion distribution in the near field. The shakeMap (Fig. 2) obtained from the 

distribution of Peak Ground Velocity at phantom stations depicts the mezoseismal area 

within the Dibra and Bulqiza districts in Albania, in accordance with macroseismic 

observations. The region of occurrence of the 2009 sequence together with the 

seismogenic region of the 1967 Dibra event, form a roughly NNE-SSW trending 

78

structure which is an active seismotectonic zone in eastern Albania constituting a threat 

for the near urban areas. 

Keywords: earthquake, Dibra earthquake, slip model, shakeMap 


79 

Figure 2: Distribution of Peak 

Ground Velocity (ShakeMap) for 

the 2009 Dibra Mw5.3 

earthquake depicting the regions 

most affected by the earthquake.




RIVER TERRACES and their AGE DETERMINATION in ALBANIA 

Rexhep KOCI 1 , Agim MESONJESI 2 , Jean-Louis MUGNIER 3 , François JOUANNE 3 , 

Julien CARCAILLET 3 Oswaldo GUZMAN 3 

1 Institute of Geosciences, Tiranë, Albania, 

2 DWM Petroleum A.G., Tiranë, Albania, 

3 Universitë de Savoie, LGCA UMR 5025 

� 

The Quaternary deposits are widely spread in Albania. These deposits fill all the Peri-adriatic 

basin of western Albania from Kopliku in the north to Vlora in the south. They are also 

fragmentary encountered in other parts of Albania like in Tropoja, Kukës, Peshkopi, Korça, 

Devolli, Kolonja, Xarë-Butrint depressions (Aliaj et al. 1996). 

The Quaternary deposits of the river valleys are represented by the sediments of the river 

terraces. From the lithological point of view, they are represented by coarse gravel sediments. 

There are identified in some levels of quaternary river terraces along the river valleys in Albania, 

which create an escalation view of the valleys itself. 

The river terraces, from the geomorphologic viewpoint, are the most beautiful views that can be 

seen along the river valleys and have been for a long time a study object for the geologists and 

geomorphologists. 

Their formation is closely linked with the periodical changes of the erosion and accumulative 

processes of the rivers as a function of both climatic changes and the character of the tectonic 

movements. This phenomena is clearly seen along the valley of Erzeni river, in Mullet-Shijak 

sector, where the river flow between two tectonic faults. 

Interactions of the tectonic development and climate agents have generated a double contribution 

to the river valleys shaping process. So, frequent tectonic movements have brought about 

formation of some terraces (Koçi 2005, Koçi et al, 2009), while, the speed of territory rise has 

determined the high between terrace levels. Meanwhile, heavy raining climate developed 

intensive erosion and produced great amount of coarse material transported by streams and 

rivers. These phenomena have occurred along the Shkumbini, Devolli, Osumi and Vjosa river 

valleys, where they cross external Albanides of the Ionian and Kruja zones, which have 

undergone almost constant speed rise and formation of the same number of terraces during the 

Plio-Quaternary. Also, the high between terrace levels of these rivers have been of the same 

order of magnitude. So, there are detected highs of 10-15m between the youngest terrace levels 

(fig 2) to 120-30m between the old terrace levels, except the case of the Devolli river, which 

have the oldest level high of 364 m (fig.3). 

81

Neo-tectonic role on formation of terrace levels is more obvious along the Erzeni river valley, 

which cross the Tirana depression and Durresi syncline separated by the Preza monocline (fig 1). 

Field surveys along the valley in question have identified three terrace levels across the Tirana 

Depression segment, whereas in the west of the Preza monocline there are described six terrace 

levels (Koçi. 2005, Koçi et al. 2009) (fig. 2). 

Fig 1:�Geoseismic profile accross the Tirana 

syncline and Preza monocline. Fig 2: Schematic cross-section on the 

medium flow of the Erzeni River. 

This drastic change of the number of the Erzen terrace levels between east and west of the Preza 

monocline resulted as a consequence of different values of the rise and fall speed between the 

cited segments. 

The formation and development of the river valleys and the river networks is related first of all 

with the geology and tectonic construction of the area where the rivers flow, as well as with the 

paleogeographic evolution of those areas. On the other hand, the formation of the terrace systems 

along the river valleys result from the combine of the geologic-tectonic, neotectonic and climatic 

factors since the beginning of the Quaternary, which were more intensive at the beginning of the 

Middle Pleistocene-Holocene time and continuous even today (Prifti K. 1990& Koçi R. 2005, 

2008) 

There are documented six river terraces up to now along the river valleys of our country. They 

are usually encountered in the middle segment of the flow and rarely in the upper segment of the 

flow. The deposits of the terraces in both of those segments have a sporadic spreading. Their 

correlation along the stream direction is usually difficult. The deposits of the terraces are usually 

encountered in one side of the river valley but in some cases they are encountered in both sides 

of the valleys (Photo 1&2, Fig. 3&4). 

Our 2002-2007 study present the identification in the field of the river terraces along the Erzeni, 

Devolli, Osumi and Vjosa valleys. A considerable number of samples were gathered in the field 

and analyzed for age determinations. Carbon 14 ( 14 C) as well as the Cosmonucloid concentration 

of Beryllium 10 ( 10 Be) method were used for age determination. The method of Beryllium 10 

( 10 Be) was used for the first time for geomorphologic determinations. The field study 

82

documented six terrace levels in the Erzeni and Devolli rivers as well as five levels in the Osumi 

(Carcaillet et al, 2009) and Vjosa valleys. In the upper flow of Vjosa river, in Greece territory, 

there are described four terraces, respectively 1000 years old for the youngest one and 150000 

years for the oldest (Lewin, J. 1989). The height of the terrace levels from the river water varies 

from 0 to 364 meters. The highest level is documented in the Devolli valley. It is located in 

Skanderbeg village at 364 meters from the water level of the river (fig. 3). 

Photo 1: View of some river terraces of the medium 

flow in the Devoll River. � 

Fig 3: Schematic cross-section of the 

medium flow of the Devoll River.� 

As for the age determination, here is what resulted using both the upper mentioned methods: 

from 200 years for youngest level up to more than 250 000 years for the oldest one. The 

youngest level is documented in the Erzeni valley while the oldest one in the valley of Devolli 

river. 

Fig. 4: (A) Panoramic view of the lower Osum showing the location of terraces units. (B) Cross section through the 

lower Osum, upstream of Berat (C) Geomorphologic map of the lower Osum, upstream of Berat. (D) 

83

Incision (m) versus ages of terrace units (ka) Breks on slope are materialized by the vertical dashed grey 

lines (J. Carcaillet et al, 2009). 

Based on age determinations for each level and their height from the river bed we found that the 

average lifting have been from 0.5 mm to 10 mm per year. Comparing the available data for the 

terrace deposits of the river valleys in Albania with those of Mediterranean area, it is concluded 

that it is a good respective correlation between the terrace units and their ages (Table 1, after 

M.G. Macklin, 2001). The data show that neotectonic movements, which affected our country 

territory during Pliocene and Quaternary period, have been of the same time with those of 

Mediterranean area. 

References 

Table 1: Age data from some rivers of Mediterranean are (after M.G. Macklin et al, 

2001).� 

Aliaj, Sh., Melo, V., Hyseni, A., Skrami, J., Mëhillka, Ll. Muço, B., Sulstarova, E., Prifti, K., 

Pashko, P., Prillo, S., 1996. Neo-tectonic map of Albania, scale 1: 200000. Archive of 

seismology Institute, Tirana, Albania. 

Carcaillet J., J.L. Mugnier, R. Koçi, F. Jouanne, 2009. Uplift and active tectonics of Albania 

from incision of alluvial tarraces. Quaternary Research 71 (2009) 465-476. 

Koçi, R., 2005. Neo-tectonic of Tirana-Durres area and its role on the terraces formation of 

Erzeni river.Archive of seismology Institute, Tirana, Albania. 

Koçi, R., 2008. Doctorate thesis: Expression of the neo-tectonic movements in terraces of some 

rivers of Albania. Archive of seismology Institute, Tirana, Albania. 

84

Koçi R., S Bushati, J.L. Mugnier, E. Perenjesi, 2009. The river tarraces-indicators of the 

neotectonic movements in Albania. 5th Congress of Balkan Geophysical Society. Belgrade, 

Serbia. 

Lewin, J, Macklin, G. M., Woodward, D. J., 1989. Late Quaternary fluvial sedimentation in 

Voidomatis Basin Epiris, northwest Greece. The Godwin Laboratory, Sub department of 

Quaternary Research, University of Cambridge CB2 3RS, UK. 

Macklin M.G., I.C. Fuller, J. Lewin, D.G. Passmore, J. Rose, J.C. Woodward, S. Black, R.H.B. 

Hamlin, J.S. Rowan, 2001. Correlation of fluvial sequences in the Mediterranean basin 

over the last 200 ka and their relationship to climate change. Quaternary Science Reviews 

2, 1633-1641. 

Prifti, K, Meçaj. N., 1990. Geomorphologic development of river valleys in Albania and their 

practice importance. Geographic Studies, Nr. 4, Tirana, Albania. 

85




From PALEOSTRESSES to PALEOBURIAL in FOLD-THRUST BELTS: 

PRELIMINARY RESULTS from CALCITE TWIN ANALYSIS in the OUTER 

ALBANIDES 

(SARANDA-KREMENARA ANTICLINES, IONIAN ZONE) 

Olivier LACOMBE (1), Nadège VILASI (2) and François ROURE (3) 

(1) Université Pierre & Marie Curie- Paris 6, ISTeP, Paris, France 

(2) Statoil, Norvège 

(3) IFP Energies Nouvelles, Division Géologie-Géochimie-Géophysique, Rueil- 

Malmaison, France 

This paper presents a first application of a new method to constrain paleoburial and 

subsequent uplift by folding in fold-thrust belts based on calcite twinning to folded late 

Cretaceous limestones from the Ionian zone in Albania. Our approach basically combines 

differential stress estimates from mechanically-induced calcite twins with the assumption that 

stress in the upper crust is in frictional equilibrium. 

Calcite twin data were collected from prefolding veins in late Cretaceous limestones from the 

Ionian zone in Albania in order to (1) determine Paleogene-Neogene stresses associated with 

the development of the major vein sets in the frontal anticlines of the outer Albanides and (2) 

estimate paleoburial of the Cretaceous reservoir rocks during pre-folding flexural subsidence 

of the foreland. The first vein set (set I) trends N140 (+/- 20) and the second set (set II) is 

oriented N060 (+/-20). Calcite twinning analysis from set I veins reveals a prefolding N030° 

extension likely related to foreland flexure; a later prefolding, NE-directed compression (LPS) 

is identified either from one or from both vein sets in the samples from the Saranda anticline; 

this NE compression is instead recorded by twinning in set II veins from the Kremenara 

anticline during late stage fold tightening. This NE compression well agrees with independent 

microtectonic data, regional transport direction and contemporary stress. 

The differential stress values related to this NE compression are combined with the hypothesis 

of crustal frictional stress equilibrium to derive first-order estimates of paleoburial of the 

Cretaceous limestones just before they were uplifted by folding. The 4 km paleoburial of 

these limestones estimated in the Saranda anticline is consistent with independent paleoburial 

estimates from stratigraphy, maturity rank of organic matter, paleotemperature 

/paleogeothermal gradients from fluid inclusions and predictions of kinematic modelling of 

the Albanian foreland. Our results therefore place reliable constraints on the amount and rate 

of vertical uplift of these Cretaceous limestones and yield a promising methodology for better 

constraining paleoburial and therefore erosion and uplift in fold-thrust belts. 

87




IDENTIFICATION of the NEOTECTONIC MOVEMENTS through 

GEOPHYSICAL METHODS in the BASIN OF ELBASAN 

Piro LEKA 1 , Petrika KOSHO 1 , Petraq NACO 2 , Fatbardha VINCANI 1 

1 

Department of Geophysics and Georisk, Institute of Geosciences, UPT. 

e-mail: p.leka@yahoo.com 

2 

Department of Georesources and Geoengineering, Institute of Geosciences, UPT. 

Elbasani’s Aquifer Basin represents one of the largest water resources of Albania. Its aquifer 

potential is conditioned by the development of extensional neotectonic system, related with 

early transversal fault of Vlorë - Ebasan - Dibër and its neotectonic regimes (Fig.1). 

41°N 

Albania 

TIRANA 

Cerriku 

Devoll's River 

20°E 

1 

Shkumbin's River 

2 

A 

Elbasani 

Elbasan's Aquifer 

Basin 

1 

B 

2 

3 3 

0 2 4 km 

Legend 

Quaternary depositions 

Transversal fault of Vlorë-Elbasan-Dibër 

Evaporite diapir of Dumrea 

Ionian's and Kruja's tectonic zones 

Tectonic sub-zone of Krasta 

Tectonic zone of Mirdita 

A- B Seismic profile 

1-1 Profile of Vidhas-Gjergjan 

2-2 Profile of Muriqan-Jagodine 

3-3 Profile Kraste-Shushice 

Fig. 1 Geotectonic position of the Aquifer Basin of Elbasani with the seismic 

and electrometric profils 

This basin is characterized by three important objects: 

� Aquifer basin of Quaternary depositions, which related with gravel terraces of 

Shkumbin’s river and represents one of the more potential drinking water resources of 

this region. 

89

� Aquifer basin of Mirdita’s zone, which related with Triassic limestones and 

extensional tectonic regime and presented evidently by surface sources. 

� Aquifer basin of Krasta’s zone, which related with Turonian - Maastrichtian 

limestones and extensional neotectonic regime, which resources drain into fluvial 

formations and into Shkumbin’s River bottom. 

Region Labinot - Fushë - Elbasan - Cërrik, at conditions of continued subsidence has incurred 

successive burying of fluvial terraces, creating the necessary conditions for the sedimentation 

of the thick gravel horizon. 

Waterbearing layer is in discordance above Ionian’s, Kruja’s, Krasta’s and Mirdita’s 

neotectonic zones with neotectonic system of faults, characterized with potential hydrological 

parameters. 

In this region, other waterbearing layers are carbonates of Mirdita’s tectonic zone of sub-zone 

Krasta, represented in depth with extensional neotectonic regime, which serve at once like 

drained planes of potential aquifer resources. 

Obtained data from the interpretation of seismic profile have helped in the conception of 

geotectonic model of Elbasan’s water basin. In such conditions is formed graben or 

cumulative depression of Elbasan, also expressed through seismic facies 0.6 to 0.2 sec 

(Fig. 2). 

Uplifting tectonic regime 

Direction of evaporite flow 

Normal fault 

Overthrust fault 

Applied drilling for oil 

Study region 

Fig. 2: Seismic Profil carried out in the N-S orientation on Aquifer Basin of Elbasani. 

For aquifer research that related with waterbearing horizons above is used the method of 

Electrometric resistivity, with array of electrical sounding -Schlumberger, AB/2 = 500 m. 

For modeling of the structure of Elbasani gravel basin in striking and in depth are carried out 

two profile (Vidhasi-Gjergjan, Muriqan-Jagodinë), but for separation of complex aquifer 

setting, that related with extensional neotectonic regime, is carried out one profile (Kraste - 

Shushice). 

Geoelectrical image 2–D of gravel horizon, with neotectonic system of faults is characterized 

complicated for the profile 1-1 “Vidhas - Gjergjan”. The third layer presents interest with 

values of electrical resistivity from 200 until 500 Ohmm, thickness from 7 until 200 m that 

presents the gravels, creating graben structure in the central part of this profile due to the 

normal slides situated with neotectonic system of faults in the valley of Shkumbini’s River 

time to time (Fig. 3). 

90

D e p t h (m) 

D e p t h (m) 

NW 


VES-1 

D-10A 

VES-2 

D-4A 

VES-3 

VES- 4 

D-3A D-4 

VES-5 VES-6 VES-7 VES-8 VES-9 

50 

0 

84 140 

900 

420 280 

230 

135 

53 

-50 

24 

38 

140 280 

63 

200 

90 

-100 

0 100 200 300 400 500 600 700 

D i s t a n c e (m) 

10 - 20 ohmm - Alevrolite - clay 

20 - 40 ohmm - Clay - sand 

40 - 90 ohmm - Sand - clay 

VES-1 VES-2 VES-3 

D-10A D-4A D-3A 

VES- 4 VES-5 VES-6 VES-7 VES-8 VES-9 

D-4 

50 

0 

-50 

-100 

-150 

-200 

0 100 200 300 400 500 600 700 


L e g e n d 

90 - 140 ohmm - Sand, alevrolite 

140 - 200 ohmm -Sand 

200 - 300 ohmm - Gravel 

D-4 

300 - 500 ohmm - Coarse-grained gravel 

Tectonic 

Applied drilling 

VES-1 

Applied VES 

Fig. 3: Geological - geophysical cross-section after VES carried out in 

the Profile 1-1 Vidhas - Gjergjan. 

Geoelectrical image 2-D of waterbearing layer for the profile 3-3 “Krastë - Shushicë” related 

with extensional neotectonic regime, is generally characterized with quasi-horizontal view of 

geoelectrical layers, in the upper part of geoelectrical section, and with the variation of 

electrical resistivity values and of thickness in the its lower part, in direction W-E (Fig. 4). 

The separation of geoelectrical layers of Mirdita’s zone with sub-zone Krasta and aftermost 

with Kruja’s zone represents the extensional neotectonics of these zones with different dip 

from the upper part to the depth. The planes of extensional neotectonics are main 

hydrogeological possible environmental of drinking supply for Ebasan city. 

91

D e p t h (m) 

D e p t h (m) 

100 

50 

0 

45 

4 

45 

-50 0 

W 

D-11 

VES-1 VES-2 

65 

7 

32 

110 

D-11 

VES-1 VES-2 

100 

50 

0 

0-10 ohmm - Sand 

VES-3 VES-4 

D-3-A 

80 

19 

36 

70 

30 

50 80 

10-20 ohmm - Clay - alevrolite 

20-30 ohmm - Breccia, gravel 

VES-5 

30 


52 

VES-6 VES-7 

100 32 

70 

14 

28 

500 1000 1500 2000 2500 3000 3500 


D-3-A 

VES-3 VES-4 

VES-5 

30 

VES-6 

L e g e n d 

15 

52 

VES-7 

VES-8 

20 

30 

200 190 

-50 

0 500 1000 1500 2000 2500 3000 3500 


30-50 ohmm - Clay - alevrolite - sand 

50-100 ohmm - Gravel 

VES-8 

100-200 ohmm - Carsted limstone 

E 

VES-9 VES-10 

VES-9 

23 

70 

VES-10 

D-11 

VES-1 

Tectonic 

Applied drilling 

Applied VES 

Fig. 4: Geological - geophysical cross-section after VES carried out in 

the Profile 3-3 Krastë - Shushicë. 

Conclusions 

1. Drillings Kozani-8, Papri-1, Maraku-1 have proved neotectonic regime of geological 

setting of Elbasn’s water basin, interpreted after seismic profile. 

2. Gravel horizon interpreted after VES in cross-section profile of Vidhas - Gjergjan 

results fragmented with normal faults and thickness of depositions that vary from 7 

until 200 m. 

3. Geoelectrical environments with variation of apparent electraical resistivity values 

after cross-section profile of Krastë - Shushicë represents neotectonic planes of 

overthrusting faults of Mirdita’s zone on sub-zone Krasta and Krasta’s zone on 

Kruja’s zone. 

References 

Melo V., 1961. Review of neotectonic movement in building of Shkumbini’s terraces in 

Elbasan -Paper sector. Geological Sciences Bulletin No. 1, Tirana. 

Naço P., Kodra A., Çina A., Bedini E., 2005. Active tectonics evaporites and permanent 

seismicity of Elbasani area. Albania 14 th Meeting of the Association of European 

Geological Society. Torino, Italy, September, 2005. 

Naço P., Bedini E., Leka P., 2006. The Aquifer Basin of Elbasani, tectonic-forming 

conditions and the problems of its management. Geological Sciences Bulletin Nr. 1, 

47-57, Tirana. 

Naço P., Bedini E., Leka P., 2006. Searching for hydrocarbons under large tectonic 

overthrusts of Albanides. Geological Sciences Bulletin No. 2, 33-42, Tirana. 

Leka P., Naço P., Vinçani F., Bedini E., 2007. Qualificative evaluation of Elbasani’s aquifer 

basin through Schlumberger electrical Soundings. Geological Sciences Bulletin Nr. 2, 

47-56, Tirana. 

92

Abstract 




Environment impact of closed copper mine in Rehova 

Skender Lipo 

Faculty of Geology and Mining, Tirana Albania 

Edmond Hoxha 

Faculty of Geology and Mining, Tirana, Albania 

In our country there are more than 30 closed mines that cause environmental pollution 

constantly beside them. One of them is the Rehova copper mine, closed 15 years ago, 

which continues to be a source of pollution and risks to the environment and population 

of this area. 

Waters going out from mine workings and the dump of the mineral 

processing plant are mixed with water flowing in Lubonja stream bringing its ongoing 

pollution, especially in the periods of intensive rainfall. 

The opencast mine stairs collapse leads to the expansion of their borders, 

destroying forests and pasture lands near the opencast area. The collapse of underground 

mining works not only damages constantly the surface of the new agricultural land, but is 

also a danger to people and livestock moving in this area. 

Large areas occupied from the opencast works are surfaces that need to be 

regenerated and turn back on forest and pasture. 

The wastes resulting from the enrichment of copper ore, has occupied a 

considerable area of land, and they pollute the waters passing through the waste mass. 

From the other side the breaks of the damp slopes risks to cause the slide of this waste 

mass over the road and agricultural lands nearby. 

The subject of this article is the assessment of the mentioned above phenomena 

and bringing of some thoughts on minimizing the damage to the environment. 

Reference 

� B. Shushku, E. Goskolli, 2009, Emergence risk situation and risk reduction at four 

Albanian tailing dams. 3 rd Balkan Mining Congress. Izmir, Turkey. 

� Lipo S., Kuka R., and al. 2007. Assessment of surface subsidence impacted from 

mining activity in coal mine Mezes. Geology and Mining Faculty, Tirana, 

Albania. 

� E. Hoxha, S. Lipo. 2005, Damage of infrastructure objects and agriculture 

production from mining activity at Rehova copper Mine. Faculty of Geology and 

Mining, Tirana, Albania. 

93

� Serafimovski T., Alderton M., Dolenc T., Tasec G., Dolenec M., 2005, Heavy 

metals in sediments and soils around the Bukim copper mine area, Geological 

Macedonia, vol. 19, Faculty of Mining and Geology, Stip, Macedonia. 

� Shushku B. Goskolli E. Hedman K. and al. 1999. Fani river environnementale 

réhabilitation programme, Final report. Geology and Mining Faculty, Tirana, 

Albania. 

94




On the LINK between OROGENIC SHORTENING and “BACK-ARC” 

EXTENSIONAL COLLAPSE in LOW TOPOGRAPHY OROGENS 

Liviu MATENCO 1 and M. DUCEA 2 

1 Netherlands Research Centre for Integrated Solid Earth Science, VU University Amsterdam, 

De Boelelaan 1085, 1081 HV Amsterdam, The Netherlands, 

2 University of Arizona, Department of Geosciences, Tucson, AZ, USA 

Classical models of orogenic evolution assume that back arc basins form in the hinterland of 

orogens, collapsing the upper plate above oceanic subduction zones. This is a common 

characteristic of all low-topography orogens of Mediterranean type, driven by the fast rollback 

of subducted slabs. This extension may take place far at the interior of the upper plate, as 

is the case in various segments of the Carpathians, but in most cases of the Dinarides, 

Apennines or Hellenides it take place superposed or far into the foreland of oceanic susture 

zones. Therefore, the term back-arc extension is misleading, as exhumation along major 

detachment zones takes place in the core of the orogen (Rif, Betics), in the accreted crustal 

material of the lower plate (Apennines, Dinarides) or even in the fore-arc (Aegean). The 

present-day Mediterranean Sea with its oceanic crust does not contain the main subduction 

zone which formed these mountain chains. Western Mediterranean formed in response to the 

rapid roll-back of the Calabrian slab, while Eastern Mediterranean is a remnant of an older 

oceanic domain, the Neotethys. The Mediterranean orogens formed in response to the 

subduction and collision of the Alpine Tethys (senso largo) during post-Early Cretaceous 

times. The Hellenides are a particular situation, where the continental crust has been scraped 

between the point of Alpine Tethys collision and Neotethys, initiating subduction in the latter. 

This means that collision has largely duplicated crustal blocks from the lower plate and has 

gradually shifted subduction zone far towards the lower plate. Amounts of lower plate 

shortening in these orogens range from >120km in the Dinarides,

� 




HYDRODYNAMIC CONDITIONS of the VISOKA FIELD TRAPPING 

Prof.. Dr. Ajet MEZINI and Prof. Dr. Ilia FILI 

IEC Visoka, Albania Branch 

The Visoka oilfield is the first carbonate filed discovered in Albania. 

From the tectonic point of view, it is situated in the Jonian Zone, in the center of “Kurveleshi” 

structural belt. (Fig.1). Being connected to the Southern periclinal of the Patos-Verbas anticlinal 

structure, which is eroded at the top, the exploration of this filed was a special case (Fig.2). 

Visoka reservoir is represented by the carbonate reservoir 

of Cretaceous-Paleogene deposits. It is a particular case 

regarding the geological and hydrodynamic condition of the 

trap formation, for the storage of oil and gas accumulation. 

This is related to the lack of flysch cover in the northern part 

of the field. In these geological conditions, the Visoka trap is 

opened in its Northern part, and the geologists question what 

are the geological and hydrodynamic factors that 

conditioned the trap formation in Visoka reservoir. In order 

to argument the trap formation in this reservoir, the data for 

the structure of Patos-Verbas, Visoka area and further in the 

south, in Ballsh up to Kemenara, were analyzed. The Visoka 

field is one of the rarest cases of oil 

Fig.1: Visoka oilfield situation and gas trap formation in the one part of an anticline 

structure. 

which is eroded at its top part. The conditions of the oil 

trapping and reservoir formation in Visoka are complicated that’s why these reservoir types are 

called “sly“ reservoirs, or hydrodynamic reservoirs. In the southern part of the structure there is the 

anticline structural form for preserving the reservoir in three principal directions. The Visoka trap 

is opened in the north direction, where it is eroded the top part of the carbonate, and lack flysch 

deposits. Miocene sandstone lie transgressively over them (Fig.2). 

After the drilling of a great number of wells in Visoka, Ballsh, and more in the south, many data 

were taken about the hydro-dynamic conditions of the waters movement in regional scale. It was 

reached into the conclusion that the hydro-chemical situation of Visoka is diversified in the saltyionic 

composition (the extension diapason is very wide) as well as in their chemical type. The 

general mineralization has very wide limits, from 0,1 gr/l (well 651 in the North) up to 36. 0 gr/l 

(well 641 in the south). Changes, and gradual transitions of the water type and general 

mineralization, in accordance to the deposits sinking, and the water metamorphosed scale, have 

been observed in the North-South direction. A type of soda bicarbonate water of increased 

metamorphosed coefficient is stored about 500 m from the eroded surface; further in the south, a 

97 

�

mineralization increase, a reduction of the mineralization coefficient, and the change of the water 

in chloro-calcitic type has been noticed. 

By analyzing the entire factual abundant material, it is very clear the presence of a hydro chemical 

deviation in the direction of the water movement, from the top part to the direction of the Southern 

pericline of anticline structure. 

Besides hydro chemical data which determine the direction of waters movement, it is also been 

made the calculation of the piezometric level of the carbonate complex of Visoka oilfield. The 

hydrodynamic measuring data about the Visoka-Ballsh region, were developed in order to 

calculate the reduced pressure on a plan surface for comparison, based on the formula: 

� 

Fig.2: Cross section in Visoka Oil Field. 

P = (L + l) ¥ + 2 where: P = the calculated pressure on a surface, L = the absolute depth of the 

well. L = static level calculated from the sea level; ¥ = specific weight of the water taken from the 

well. The piezometric level of some wells in Visoka was calculated based on these data (see table). 

Both the piezometric level and pressure values prove movement of water from the eroded surface, 

well 651, in South direction, according to the above line of wells. A full compliance between the 

hydro-chemical and hydro-dynamic indicators has been observed in the Visoka field. 

Well Reduced Piezometric 

pressure level 

651 208.3 146.1 

649 207.4 135.2 

G-16 205.9 121.7 

Ba-6 206.4 131.2 

Ba-13 205.9 123.3 

Ba-8 206.1 123.9 

Ba-15 206.4 127.06 

Ba-1 205.3 115.4 

Gr-3 204.5 108.4 

Visoka oilfield proves the basic principle of the 

hydrogeology, that the hydrochemistry is a 

consequence of the hydrodynamic, and the last one is 

the result of the geological-structural conditions. In 

these hydro-dynamic conditions, the Oil-Water contact 

in Visoka is not horizontal. It is inclined in Southern 

direction, or in the direction of water movement (636, 

1050m, G-180, 1840m), as well as in the West direction 

(well 627 1325m), and in East (G-238 1680m). 

The inclined oil-water contact in Visoka is the 

synthesis of the coordination of the active underground 

waters to the oil reservoir, as well as their role during 

the paleo-hydrogeological development in creating the 

conditions for the reservoir preservation. By analyzing all the geological, hydrodynamic, hydrogeological, 

physical, chemical, biodegrading, lithological, stratigraphic, and tectonic data, we think 

that besides the principal factor in the trap formation of Visoka, some other factors have also 

played an important role, such as: 

According to hundreds of exploration and exploited wells in Visoka field it is been observed a 

noticeable heterogeneity of the rock property features between the wells, particularly regarding the 

permeability. This heterogeneity and the anisotropy have influenced in preventing the oil migration 

98 

�

from the Southern part to the direction of the top of the structure. Cases of lack of communication 

from one well to another, and between two double wells, are numerous in Visoka oil field. Such 

collector barriers are also known in other carbonate oilfields in our country, such as the case of the 

direct contact of western flank of Mollajt to the Eastern flank of Selenica. At the zone of dry wells 

G-56, G-57, G-58 and 616, which represents the transition from the Central zone to the Northern 

one, there is a noticeable lack of communication, low permeability,(Dry wells), which has 

prevented the oil migration in the Northern direction. 

The Upper Miocene mollassic deposits lie transgressively over the eroded part of the carbonate, of 

the Patos-Verbasi anticline structure (Fig.2). It is an undisputable fact that a great quantity of oil 

and gas reserves has migrated from the eroded carbonate to the sandstone reservoir of these 

deposits, and has saturated them, up to their outcrop in the surface in South, in Patos. During the 

geological period Upper Miocene-Quaternary, at the part where these deposits come out to the 

surface, the oil is oxidized, the light fractions move away, and are turned into bitumen. In the 

current situation these layers are bitumen-bearing layers. Bitumen has served as a screen (seal) to 

prevent further migration of the oil. So, it is created a natural coverage, or bitumen screen, which 

has not allowed the further migration of the oil in the newest geological times. 

Sandstone deposits are situated in stratigraphic discordance on the eroded surface of the carbonate, 

or of the argillites, of the Upper Miocene. Being in direct contact on the eroded carbonate, these 

deposits communicate with the last ones which they are supplied with oil. The presence of the 

argillaceous lithology, or the compact sandstones, in the southern part of the eroded surface makes 

impossible the oil migration to this part of the structure from the southern part of the field. 

The oil of Visoka oil field is very viscous, of specific weight 0.990-1.02 gr/cm 3 . This oil is 

migrated by the early fluxes of migration, Lower Oligocene and on. During the geological periods 

thanks to the different structural and geological conditions are moved away the lightest oil 

fractions. Also, being in contact with the water that moves through the eroded surface of the 

carbonate, the oil is oxidized. Its swimming force is too small, or zero, when the specific weight is 

almost the same to the water. In these conditions the movement has been very difficult, or its 

migration from Visoka reservoir to the direction of the top-most part. 

The tectonic plan of Patos-Verbas has changed after the erosion of its top part. The northern part of 

the carbonate eroded surface is under the absolute depth 2000 m today, or lower than the carbonate 

top in Visoka. This change of the tectonic plan has made possible the fluids movement and reestablishment 

in this structure. 

All these factors together have made possible that Visoka oil field is preserved in the current 

situation of the hydro-dynamic equilibrium of fluids. However, a great quantity of oil reserves has 

migrated from this structure. The oil field has been created, destroyed, and recreated in the 

youngest geological periods. 

Conclusions 

The Visoka field represents a special case of the trap formation of hydrodynamic type, formed in 

the southern pericline of an anticline structure. 

The hydro-dynamic and hydro-chemical measurements of the wells in Visoka and Ballsh prove the 

existence of a pressure gradient and the underground waters movement from the raised part of 

Patos-Verbas structure in its plunging direction. The water movement in this direction has made 

possible the preservation of the oil reservoir in Visoka. 

� 

99 

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Besides the hydro-dynamic factors, in the preservation of Visoka reservoir have influenced also 

other factors such as: geochemical, collector, permeability and the geological-structural 

framework. 

The oil-water contact of the field is slope and it falls in the South direction with a smaller angle 

than the top carbonate. 

The hydrodynamic and hydro-chemical studies are equally important as the tectonic and 

stratigraphic ones for exploring the new reservoirs, especially in hydro-geological complicated 

conditions. 

References 

Abhijit Y. Dandekar, 2006. Petroleum Reservoir Rock and Fluid Properties. 

Alimonti C., 2002. Quantifying matrix-to fracture connectivity in fractured reservoirs. 

Aliscioni A., 2002. AAPG Hedberg Conference, May 14-18, 2002, Palermo. 

Cosentino L.,2001. Integrated Reservoir Studies. Edition TECHNIP. 

Dhamo Ll. etj. 

Djebbar T. 2004. Petrophysics. Theory and practice of measuring reservoir rock, and transport 

properties. 

Donaldson E. 

Gambini R., 2002. Mondello, Sicily, Italy, 2002. 

Kadilli F. etj., 1967. 

King H., 1974. Oil trapping in the hydro-dynamic conditions. AAPG Bull., 

37, Nr 8. 

Moore B., 2007. Carbonate Reservoirs. Porosity Evolution and Diagenesis, Developments in 

sedimentology, 55. Elsevier. 

Pano Dh., 1989. Optimal Criterionsof Visoka Oil Field exploitation. 

Ranxha S. etj.,1989. 

Sahatçiu R.,1967. Report about reserve calculation on Visoka oil field. 

Sako L.,1972. Exploitation Analysis of Visoka oil Field, Fier. 

Shtrepi P., 1980. Complex of indicators for study of Hydro-dynamic oil fields. IGJN Fier, Albania. 

Shtrepi P.,1982. Hydro-geological characteristics of oil fields in Albania. IGJN, Fier, Albania. 

Taylor & Francis. 

� 

100 

�




FOUR DIMENSIONAL GEOLOGICAL EVOLUTION 

of the EASTERN TYRRHENIAN MARGIN 


GEODYNAMIC IMPLICATIONS 

Alfonsa MILIA (*), Eugenio TURCO (°) and Maurizio M. TORRENTE ( # ) 

(*) IAMC-CNR, Naples, Italy; e-mail: alfonsa.milia@hotmail.it 

(°) 

( # ) DSGA, University of Sannio, Benevento, Italy; e-mail: torrente@unisannio.it 

The Tyrrhenian Sea is a Neogene back-arc basin formed by continental extension at the rear of the 

eastward migrating Apennine subduction system. It is characterized by deep central basins 

(Magnaghi-Vavilov and Marsili) containing elongated volcanoes and deep peri-tyrrhenian basins 

filled by thick sedimentary successions. Even if numerous studies were based on data in the deep 

central basins (e.g. Kastens et al, 1988; Sartori, 1990) the study of sedimentary basins located along 

the margin of the Tyrrhenian Sea reconstructed a detailed chronostratigraphic framework and a 

four-dimensional reconstruction of the fault systems (e.g. Milia and Torrente, 1999; Milia et al., 

2009). 

We studied the Eastern Continental Margin of the Tyrrhenian Sea, between the 42° and the 38° N 

parallel (Latium-Campania-Calabria margin, Fig. 1) characterized by deep sub-basins filled with up 

to 3-5 km of Plio-Pleistocene sediments. The geologic evolution of these basins have been 

established on the basis of a large amount of seismic reflection data with different resolution and 

penetration, exploration wells, core data and onshore data. The interpretation of the seismic 

reflection profiles, based on seismic/sequence stratigraphy and structural analysis methodologies, 

permitted to determine timing and kinematics of the faults affecting the Eastern Tyrrhenian Sea. 

During the Upper Pliocene-Lower Pleistocene the Gaeta Basin (Latium) was affected by an E-W 

extension that formed a deep triangular graben bounded by approximately NNE- and NNWtrending 

normal faults (Iannace et al. 2010). Simultaneously, off Calabria, originated the Paola 

Basin, an asymmetric extensional basin controlled by E-W normal faults and more than 2 km thick 

of sedimentary succession (Milia et al., 2009). During the Middle Pleistocene, between 700 and 400 

ky, the Campania margin was affected by NE trending half grabens filled with up to 3 km of clastic 

deposits associated to a NW-SE directed extension (Milia 1999, Milia and Torrente, 1999), while 

the Paola Basin was characterized by a remarkable folding associated the activity of a left lateral 

trascurrent fault zone and the deposition of approximately 1 km of sin-kinematics sediments. Over 

the last 400 ky on the Campania Margin the extension direction changed from SE to ESE and the 

prexisting fault systems were reactivated during the emission of large volume ignimbrite eruptions 

(Milia and Torrente, 2007; Torrente et al., 2010). At the same time a right lateral trascurrent fault 

zone affected the Paola Basin and ca 1 km of deep water sediments were deposited in a N-S 

oriented basin depocenter. 

Our four dimensional reconstruction of the sub-basins permits to point out the structural styles of 

the Plio-Pleistocene phases of basins development. These structural styles can be related to opening 

episodes of the Tyrrhenian Sea and the three phases of the basins developments furnish a constraint 

to the reconstruction of the Plio-Pleistocene evolution of the Eastern Tyrrhenian Sea. 

1) During the Upper Pliocene-Lower Pleistocene the opening of the Gaeta Basin (Latium) and of 

the oceanic Marsili Basin occurred; contemporaneously an extension zone (Paola Basin) between 

101

these basins formed. 2) During the Middle Pleistocene a rifting episode took place in the Campania 

margin that formed NE trending half grabens while the extension stopped in the Gaeta Basin. 3) 

Over the last 400 ky the Eastern Tyrrhenian margin the extension in the Campania Margin is 

associated to an intense volcanism and a dextral shear zone characterize the boundary between the 

deep Tyrrhenian basin and the Eastern Tyrrhenian continental Margin (Milia et al., 2009; Milia et 

al., 2010). The results of this geologic processes is the individuation of a breakway zone located in 

the Campania Margin that bound a microplate migrating toward the SE. 

Fig. 1. Seafloor morphology of the Tyrrhenian Sea (Marani et al., 2004) and location of the study 

area. 

References 

Iannace P., Massa B., Milia A., Torrente M.M. (2010) 3-D modeling of the structural features of 

Gaeta Bay (Eastern Tyrrhenian Sea margin). Rendiconti online Soc. Geol. It., Vol. 10, 73-75. 

Kastens, K.A., Mascle, J. and Others, O.D.P. (1988) Leg 107 in the Tyrrhenian Sea: insights into 

passive margin and backarc basin evolution. Geol. Soc. Amer. Bull. 100, 1140-1156. 

Marani M.P., Gamberi F., Bortoluzzi G., Carrarra G., Ligi M., Penintenti D. (2004) Seafloor 

morphology of the Tyrrhenian Sea, Scale 1:1,000,000. Included to Mem. Descr. Carta Geol. 

Italia, 44. 

Milia, A. 1999. Aggrading and prograding infill of a pery-tyrrhenian basin (Naples Bay, Italy). 

Geo-Mar. Lett., 19, 237-244. 

Milia A. and Torrente M.M. (1999) Tectonics and stratigraphic architecture of a pery-Tyrrhenian 

half-graben (Bay of Naples, Italy). Tectonop., 315, 297-314. 

Milia A. and Torrente M.M. (2007) The influence of paleogeographic setting and crustal subsidence 

on the architecture of ignimbrites in the Bay of Naples (Italy). Earth Planet. Scie. Lett., 263, 

192-206. 

102

Milia A., Turco E., Pierantoni P.P. and Schettino A. (2009) Four-dimensional tectono-stratigraphic 

evolution of the Southeastern peri-Tyrrhenian Basins (Margin of Calabria, Italy). Tectonoph., 

476, 41-76. 

Milia A., Morabito S., Passero S., Ruggieri S., Turco E. (2010) Tectonics and Geomorpholgical 

processes between Sirene and Sartori Lineaments (Eastern Tyrrhenian Sea). Rendiconti online 

Soc. Geol. It., 10, 83. 

Sartori, R., 1990. The main results of ODP Leg 107 in the frame of Neogene to Recent geology of 

perityrrhenian areas. In: Kastens,K.A., Mascle, J., et al. (Eds.), Proceedings of the Ocean 

Drilling Program. Scientific Results 107, pp. 715– 730. 

Torrente M.M., Milia A., Bellucci F., Rolandi G. (2010) Extensional tectonics in the Campania 

Volcanic Zone (eastern Tyrrhenian Sea, Italy): new insights into the relationship between 

faulting and ignimbrite eruptions. Ital. J. Geosci. (Boll. Soc. Geol. It.), 129, 1-19. 

103

104




TRIASSIC-JURASSIC VOLCANO-SEDIMENTARY FORMATION in ALBANIA and its 

RELATION with the MIDDLE JURASSIC MIRDITA OPHIOLITE 

Ibrahim MILUSHI 1 , Avni MESHI 2 and Gjon KAZA 1 

1 Institute of Geosciences, Polytechnic University of Tirana, Albania 

2 Faculty of Geology and Mine, Polytechnic University of Tirana, Albania 

Volcano-sedimentary formation (VSF) of the Middle Triassic to lower Jurassic ophiolite is 

relatively widespread in Albania. The formation, as a non-continuous narrow belt, extends for 

more than 300 km along the western and the eastern margins of the Middle Jurassic ophiolite. In 

most cases VSF is “sandwiched” between Middle Jurassic ophiolite massifs in the hanging-wall 

and Triassic-Jurassic sedimentary formations of the former continental margin in the foot-wall. 

At the thrust contact between VSF and ophiolite, which is outlined by serpentinite, a 

metamorphic sole represented by blue schist, mica schist and amphibolites has developed. 

In places, VSF crops out even as tectonic windows inside the Middle Jurassic ophiolite, implying 

it is extending widely underneath the ophiolitic massifs. 

Thickness of VSF is generally 150-300 m, but in some areas it reaches up to several hundred 

meters: the Porave over 800 m, 600 m in Karma, in Rubik up to 600 m, etc. 

It consists of MORB-type basalts, radiolarian cherts and argillaceous-siliceous and siliceous 

schist. In different areas, different facies are predominant: for example basalt dominates in 

Porava, Karma and Rubiku, while schists and radiolarian cherts are more developed in Gjegjani, 

Surroj, etc. 

Basalts are represented by pillow and aglomeratic lavas, rarely by massive basalts. They belong 

to tholeites rich in TiO2 ranging from 1.1 to 2.2 % often showing andesitic tendency. According 

to the ages determined by the radiolaria of the cherts, VSF belongs to a wide age range from Mid 

Triassic to Lower Jurassic. 

VSF formed after the continental break-up that started in Middle Triassic and kept on during the 

Late Triassic up to Early Jurassic. In the Middle Jurassic, the Mirdita ocean became again active, 

accounting for the development of the Jurassic Mirdita ophiolite During the last part of the 

Middle Jurassic, after the intraoceanic suprasubduction event, the Middle Jurassic ophiolite 

massifs were thrust over the Middle Triassic-Lower Jurassic VSF. Consequently, the 

metamorphic sole originated. Later, under the compressional regime which took place in Late 

Jurassic, VFS together with ophiolite massifs were thrust over the former continental margin. 

In most cases VSF is folded and intensely sliced, incorporating even fragments of a “block in 

matrix” mélange. 

Flysch of Tithonian-Valanginian unconformably covers the formations of former continental 

margin, VSF and ophiolites. 

VSF is rich in massive sulphide ores. These mineralizations are different from those related to 

the volcanic sequences of the Middle Jurassic Mirdita ophiolite. 

105

106




BIOSTRATIGRAPHY of the TARBUR FORMATION, ZAGROS BASIN 

I. Maghfouri MOGHDDAM 

Department of Geology, faculty of Sciences, Lorestan university , Fakol aflak, khorram abad, 

Iran 

E-mail: iraj mmms @ yahoo.co.uk 

phone:++ 98661 2200272 

Fax:++ 98661220285 

The Tarbur Formation is a predominantly carbonate lithostratigraphic unit that crops out in 

the Zagros Basin, between the main Zagros reverse fault and the High Zagros and east of 

Sabzpushan Fault. This formation was studied from biostratigraphic point of view at four 

measured sections (Robut, Chumsangar, Balghar and Sarvestan). 

Microbiostratigraphical data mainly based on foraminifera which indicate Early- Middle 

Maastrichtian age for deposits of the Tarbur Formation at Sarvestan and Middle Maastrichtian 

for Balgar, Robat and Chamsangar sections. 

Keywords: Tarbur Formation, biostratigraphy, Maastrichtian, Zagros. 

107

108

ILP�TASK�FORCE�on�SEDIMENTARY�BASINS� 

2010�International�Workshop� 

November�7�12,�2010,�Tirana�(Albania)� 

The ENGINEERING GEOLOGICAL and GEOPHYSICAL STUDIES for LAND-USE 

PLANNING in ADRIATIC COASTAL PLAIN-DIVJAKA, ALBANIA 

� 

Ylber MUCEKU, Jani SKRAMI, Edmond DUSHI, Mehmet ZAÇAJ 

Institute of Geosciences, Polytechnic University of Tirana, Albania 

In this paper are presented the results of the engineering geological investigation carried out 

in the Adriatic Coastal Plain of Albania, Divjaka area. The studied area extends in west of 

Lushnja town, along of the Adriatic coastal plain from Shkumbini to Semani Rivers delta. It’s 

one of the most attractive place in Albania, because of there are several wonderful beaches, 

which have take much interest of many designers companies and institutions related to 

touristic center development. That is the motivation, why last years we have carried out the 

geotechnical and geophysical investigations, results of which are presented in this paper. 

From these works an engineering geology zoning map on scale 1: 10 000 is completed. For 

that are done 35 geotechnical drillings with 20.0m up to 30.0m and many seismic 

measurements, as well as, are taken respectively 78 and 57 disturbed and undisturbed soils 

samples. They are taken in different depth of the boreholes from 1.0m up to 30.0m and are 

analyzed in the laboratory to determine of physical and mechanical parameters as bulk 

density, grain size distribution, Atterberg’s limits, moisture content, specific density, dry 

density, porosity, porosity coefficient, shear strength and oedometer module. Also, in 

compilation of the engineering geology map are taken under consideration the oils boreholes 

carried out for oils exploration purpose, which are 500-1000m deep. Besides of the boreholes 

are used and seismic methods, which have helped to determine the soils thickness, 

underground waters, as well as the structural and neotectonic elements. So, for investigation 

of soils deposits in Divjaka area a lot of seismic velocities measurements on surface and in 

boreholes have been carried out. For this are completed 40 points of seismic measurements 

represented by the velocity of shear and longitudinal waves (Vs and Vp). Furthermore, in the 

western part of Divjaka town, are taken the velocity measurements of shear and longitudinal 

waves (Vs and Vp) in the depth of the boreholes by using the “down-hole” seismic method. 

According to geology Divjaka area is part of the Western Lowland of Albania and it includes 

in Preadriatic Depression. It is built by Mio-Pliocene molasses and Quaternary deposits. 

Whereas, related to geological structure the Preadriatic Depression is built by some Mio- 

Pliocene wide synclines and linear relatively narrow anticlines as Divjaka anticlines, which 

are superimposed over thrust and back thrust faults. The Mio-Pliocene anticline folds do not 

outcrop with all their elements, whereas the synclinal structures are buried from soils of 

Quaternary deposits. The positive structures of the western coastal part are well expressed on 

the relief; the anticlines build hills, while the synclines are covered by Holocene deposits. The 

soils are represented by coastal, alluvial, lagoons and swamps deposits. They have the 

thickness varied from 20.0-30.0m (eastern part) and 300.0–350.0m (western part). The coastal 

deposits consist of sands and silty sands and extend to west of the studied area, along the 

109

Adriatic coastline. The alluvial deposits (delta of the River Shkumbini) are located in the 

northern part of the study area and represent by combination of loam and sand layers. 

Whereas, the lagoons and swamps deposits are found in west and southwest. They are formed 

as a result of interaction of the River Shkumbini with sediments discharged at the coast. 

Swamp deposits were characteristic of a past, semi-arid landscape of the Holocene age and 

are located in west of studied area. All above mentioned soils are situated over of molasses 

rocks. From the hydrogeology point of view the observed zone is constructed by two 

complexes, which are soils (Quaternary deposits) and rocks (Molasses rocks). The lower and 

middle part of the soils deposits are built by gravels and in upper part by coarse sands, which 

are intercalated by thin layers of silts. The underground waters in the region, part which is the 

studied area are related to gravels and sands formations, which formed a rich aquifer 

according to water bearing. The main water recourse of these formations is Shkumbini River. 

The second complexes represent by the molasses rocks that built from the layers combination 

of claystones, siltstones and sandstones rocks. The claystones and siltstones are very poor to 

water bearing, whereas the sandstones formations form a good aquifer to underground water 

reserves. During fields works is systematically taken the measurements of underground water 

levels. This procedure is repeated each month for three month in row and concluded that 

underground water table is 0.5-1.0m up to 3.0-5.0m deep. 

Based on morphology features the studied area is divided in flat morphological unit and hills 

morphological unit. 

The flat morphological unit represents by the Adriatic flat plain with elevation varies from 

0.5-2.0m (western part) to 5.0-7.0m (eastern part). Along of this zone from east to west 

direction have established their valleys with “U” shape Shkumbini and Semani rivers and 

central part is located Karavasta lagoon. 

Hills morphological unit is located in east of studied area. It is represented by Divjaka hills 

chain. The elevation of this morphological unit range from 80 m up to 120 -150 m. The 

morphological unit is composed by claystones, siltstones, sandstones and conglomerates 

rocks. The hills slopes have inclination range from 6 o -10 o up to 15 o -30 o and some place more. 

Engineering Geology Zoning-From fields and laboratories data analysis an engineering geology map 

on scale 1:10 000 was compiled. From this analysis the study area is divided in the following 

engineering geology zones: 

· The engineering geology zone of the silts and sands combination with thickness 10-30 m and 

underground waters below 5 m. 

· The engineering geology zone of the silts and sands combination with thickness 30-100 m and 

underground waters range from 3 m up to 5 m. 

· The engineering geology zone of the fine to medium sands-beach sands and seas sands with 

thickness exceed 100 m and underground waters range from 0.5 m up to 3 m. 

· The engineering geology zone of the peat–loam-sands combination with thickness exceeds 

100.0m and underground waters 0.5 m. 

· The engineering geology zone of the loam-sands combination-alluvial fan of Shkumbini River 

with thickness exceeds 100 m and underground waters range from 0.5 m up to 3 m. 

· The engineering geology zone of the diluvium deposits coverage, represent by silts and clays 

with thickness 1.5-5 m. 

· The engineering geology zone of the soft rocks, claystones. 

In the end, we emphasize the studied area is generally built by soils with low geotechnical 

properties, which in case of urban development have necessary needs of taking of engineering 

measures to soils foundation improvements. 

110




LOW TEMPERATURE THERMOCHRONOMETRY in INTERNAL ALBANIDES: 

QUANTITATIVE CONSTRAINTS on EXHUMATION RATE and TECTONIC 

IMPLICATIONS 

Bardhyl MUCEKU (1) , Georges H. MASCLE (2) Peter van der BEEK, (2) Matthias 

BERNET (2) , Peter REINERS (3) , and Artan TASHKO (1) 

1 Polytechnic University of Tirana, Rruga Elbasani, Tirana, Albania. 

2 Laboratoire de Géodynamique des Chaînes Alpines, Université Joseph Fourier, BP 53, 38041 Grenoble, 

France. 

3Department of Geosciences, University of Arizona, Tucson, AZ 85721, USA. 

*corresponding author, email: bmuceku@gmail.com 

Albania occupies a central position within the Dinaro-Hellenic alpine mountain belt. This 

orogen is characterized by three fundamental components: a Western Fold-and-Thrust Belt 

(External Albanides), a Central Belt characterized by the occurrence of ophiolitic nappes, and 

an Eastern Complex (Internal Albanides). The internal Albanides were affected by pre- 

Tertiary tectonics, and in the external Albanides the deformation started during the Eocene. 

This deformation is related to subduction of the Apulian plate beneath the Eurasian plate. 

Fission-track (FT) and (U-Th)/He analysis on apatite and zircon permits to better constrain the 

thermal history of this mountain belt. Apatite (U-Th)/He ages in the western and northern 

Internal Albanides range from 55 Ma to 24-35 Ma, being in strong contrast with younger 

apatite (U-Th)/He ages of 4.5 to 9.3 Ma obtained for the eastern Internal Albanides. All of 

these results are in good agreement with AFT ages from the same areas. The observed eastwest 

trend with older cooling ages in the west and younger cooling ages in the east across the 

Albanides is also reflected in zircon (U-Th)/He ages that range between 80-100 Ma in the 

north-western Internal Albanides, and 20-50 Ma in the eastern Internal Albanides. Only the 

higher-temperature zircon FT ages do not show any significant differences on both sides of 

this area. Thermal modeling based on the available low-temperature thermochronologic data, 

in particular the apatite (U-Th)/He ages, provide clear evidence for a phase of rapid 

exhumation of the eastern Internal Albanides around 3-6 Ma, reaching a rate of about 1.2 

km/m.y., while the western Internal Albanides record much slower exhumation since the 

Eocene (< 0.1 km/m.y.). 

The strong lateral gradient in rock uplift rates implied by the thermochronologic data suggests 

accommodation of this variation by faulting. The present-day structure of the Albanides, with 

major west-dipping faults forming the boundary between the Mirdita and Korabi zones and 

occurring within the Korabi zone constrains such faulting to be extensional on reactivated 

NE-SW trending former thrust fault systems. 

We suggest that late Oligocene to early Miocene crustal thickening and shortening in the 

Albanides changed to an extensional regime in the eastern part of the orogen at about 6 Ma. 

Our thermochronological data indicate that rocks of the Korabi zone where exhumed from 2-3 

km depth during this late extension phase. These results are in good agreement with regional 

structural and stratigraphic information. 

111

112




ALBASEIS, RISK ASSESSMENT and SEISMICITY of ALBANIA 

Betim MUCO 

General Dynamics Inc./ IRIS, USA 

The project “Seismotectonics and Seismic Hazard Assessment in Albania” was the first 

NATO project for Albania. It has been a joint project between the Seismological Institute of 

Academy of Sciences of Albania and the Department of Geophysics of Aristotle University of 

Thessaloniki, Greece. This collaboration was an excellent example of the relations that 

European Union cultivated in the Balkan area through the Stabilization and Association Pact 

and other programs. 

Earthquake occurrence is most significant natural hazard in Albania. After the collapse of 

Communist regime and the opening of the country, a boom of constructions launched in 

Albania and it is still a developing sector. The eventual implementation of seismic hazard 

studies into the construction designs will prevent loss of life and property. On the other hand, 

the oil and gas are the main natural resources of the country. The seismotectonic analysis and 

the identification of active tectonic faults and the study of the geophysical potential fields are 

closely connected with the effective exploitation of these resources. 

These two pillars composed the structure of the entire project which started in January 1999 

and ended in December 2003. 

During these four years of effective collaboration many significant publications were 

produced and contributed to the development of modern Seismology and Geophysics in 

Albania as well as to the better understanding of the oil and gas basins and their exploitation. 

A complete catalogue with more than 20,000 events has been obtained for the period 1964- 

2000 and all epicenters were relocated (Fig. 1). Earthquake locations have been improved 

using refined velocity models obtained from tomography and the Moho depth distribution has 

been mapped. Earthquake focal mechanisms have been determined using advanced techniques 

and plate motion models have been tested. The project provided important results on both 

deterministic and probabilistic analysis of seismic hazard assessment of Albania, the first 

complete studies of this kind in the country (Fig.2) 

The extensive study of potential fields, the distribution of gravitational and geomagnetic data 

provide significant contribution to the interests of research and exploitation organizations of 

the hydrocarbon reservoirs in Albania. 

With about two thirds of the budget going to Albania, this project helped to enhance the 

scientific infrastructure of the Seismological Institute directly and indirectly. The direct 

impact was the use of project funds for purchasing computers, printers, scanners, software, 

spare parts, instruments of seismic monitoring and seismological engineering. 

A local computer network has been established and the Internet connection has been for the 

first time available for all the scientific staff of the institute since 1999. A considerable 

number of Albanian scientists had the chance to be trained in well respected Earth Science 

Organizations in Thessaloniki, Rome, Trieste, and Skopje. Moreover, theNATO project 

provoked the increase of funding to the Seismological Institute through the Academy of 

Sciences of Albania for the modernization of seismic monitoring in the Albanian 

Seismological Network. A digital network and a satellite transmitting VSAT network were 

constructed during and in the wake of the ALBSEIS project. 

113

The first project of "Science for Peace" program of NATO for Albania has been a great 

contribution to the development of seismology in this country. 

Fig. 1 Relocated epicenters for the Albanian and 

surrounding region of the period 1964-2000. 

114

Fig. 2 PGA distribution for 90% of non-exceedance on 50 years 

115

116




THERMAL EVOLUTION, HYDROCARBONS GENERATIONS and HC POTENTIAL 

of TRIASSIC and LIASSIC CARBONATE RESERVOIRS in the IONIAN ZONE 

(ALBANIA) 

(STUDY BASED on OUTCROPS and WELLS). 

Prof.Asc.Dr.Kristaq MUSKA 

Polytechnic University Tirana 

kristaqmuska@yahoo.fr 

(Poster presentation) 

SOURCE�ROCK�LEVELS� 

Several source rock levels have been observed in outcrops of different zones in Albanide. In the 

Ionian zone: black shale intercalations of Late Triassic from thin centimeters to thick organicrich 

layers, comparable to those of Burano formation (Early Triassic) in Southern Italy, have 

been encountered. 

Photo.1: Mali i Gjërë. Source rock levels 

In Cika belt Early Triassic source rocks have a 

gross thickness of up to 15m. Based on the 

outcrop samples TOC=0.1-38% have been 

recorded for these source rocks. In the basal 

Jurassic similar intercalations with higher TOC 

values (up to 52%) have been recorded. In the 

Shpiragu-1 well a 600m gross interval was 

recorded with posidonia shale interlayer. In 

Middle and Jurassic and also in the Late Jurassic some further thin, organicrich shale 

intercalations with maximum TOC =9% have been evidenced. A couple of thicker bituminous 

shale/limestone intervals are known from the Lower Cretaceous with maximum TOC =27% have 

been recorded. They probably correlate with similar organic-rich deposits from Peri Adriatic 

carbonate platform of Former Yugoslavia. 

117 

Photo 2: Organic- rich shale 

SOURCE�ROCK�QUALITY� 

Good to excellent quality, of type I/II source 

rocks are present in the Upper Triassic, Lower 

Jurassic and Lower Cretaceous of the Ionian 

Zone. The Toarcian, Middle Jurassic and

Upper Jurassic of the Ionian Zone contain poor to good quality type I/II source rocks for oil. 

SOURCE�ROCK�MATURITY� 

The outcrops Upper Triassic and Lower Jurassic source rock levels in the Ionian zone show 

mature for oil generation (VR/E 0.53-0.88). 

THERMAL�EVOLUTION�and�HYDROCARBONS�GENERATIONS� 

Thermal evolution was made by 1D modeling with GENEX-GenTect software. These models 

were calibrated using the organic matter maturity parameters (Tmax, vitrinite). 

Fig.1: Model calibration. 

The paleotemperatures measured in the fluid 

inclusions were compared with the temperatures 

calculated by the model. In this way, it has been 

possible to determine the reservoir cementation time 

period. 

Fig.2: Evolution of the formations temperature with 

time and the burial. 

My results show that surface outcrops of Triassic- 

Liassic dolomitic reservoirs never reached 

temperature in excess to 80°C, thus accounting for 

dominantly early diagenetic features. However, 

potential reservoirs in deeper, still untested horizons 

are likely to have reached temperatures in the range 

of 120-140°C, and thus, are likely to display highly contrasted paragenetic assemblages, 

involving the development of hydrothermal dissolution or high temperature dolomitic cements 

(saddle dolomite), two processes known elsewhere to develop secondary porosity. 

Fig.3: Total quantity of hydrocarbons generated 

118

KEYWORDS: source rock levels, TOC, 1D modeling with GENEX-GenTect software, 

hydrocarbons generated, secondary porosity 

REFERENCES 

Albpetrol, 1993. Petroleum exploration opportunities in Albania: 1st onshore licensing round in 

Albania. Publicity brochure, Western Geophysical, London. 

Curi F., 1993. Oil generation and accumulation in the Albanian Ionian basin. In Spencer A.M., 

ed., Generation, accumulation and production of Europe's hydrocarbons, Springer, EAPG 

Spec. Publ., 3, 281-285. 

Curi F., Stamuli T., Dule A. et Gjermeni M., 1990. Geochemical conditions of hydrocarbon 

generation, migration and accumulation in carbonate and molasse deposits. Nafta dhe 

Gazi, Fieri, 97-111. (in Albanian) 

Danelian T. et Baudin F., 1990. Découverte d'un horizon carbonaté, riche en matière organique, 

au sommet des radiolarites d'Epire (zone ionienne, Grèce): le Monte de Paliambela. C. R. 

Acad. Sci., Paris, 311, II, 421-428. 

Danelian T., De Wever P. et Vrielynck B., 1986. Datations nouvelles fondées sur les faunes de 

Radiolaires de la série jurassique des Schistes à Posidonies (zone ionienne, Epire, Grèce). 

Rev. Paléobiol., Genève, 5, 1, 37-41. 

Diamanti F., Sadikaj Y., Zaimi L., Tushe I., Gjoka M., Prifti I. et Murataj B., 1995. Hydrocarbon 

potential of Albania. In 1965-1995, 30 years Oil and Gas Institute, Albpetrol ed., 300 p. 

Frasheri A., Kapedani N., Lico R., Canga B. et Jareci E., 1995. Geothermy of External 

Albanides. In 1965-1995, 30 years Oil and Gas Institute, Albpetrol ed., 300 p. 

Muska K., 2002. Termicité, transferts et diagenese des reservoirs dans les unités externes des 

albanides (Bassin ionien). Thèse de Doctorat, Paris VI. 

Roure F., Lafargue E., Müller C., Fili I., Muska K., Nazaj S., Seiti H., Cadet J.P., Bonneau M. et 

Mio I., 1998. Evolution structurale et pétrolière des Albanides externes. Résultats de la 

modélisation Thrustpack et des analyses géochimiques complémentaires. Rapport IFP 

report 44888 pour OGI. (confidentiel). 

Roure F., Nazaj S., Muska K., Fili I., Cadet J.P. et Bonneau M., 1999. Kinematic evolution and 

petroleum systems: an appraisal of the Outer Albanides. In McKlay K., ed., Thrust 

tectonics 1999, in press. 

Roure F., Prenjasi E. et Xhafa Z., 1995. Petroleum geology of the Albanian thrust belt. Guide 

book to the Field Trip 7, AAPG, Nice, 50 p. 

Roure F. et Sassi W., 1995. Kinematics of deformation and petroleum system appraisal in 

Neogene foreland fold-and-thrust belts. Petroleum Geosciences, v. 1, p. 253-269. 

119

120




The MECHANICS of THRUST TECTONICS, the EVOLUTION of the 

ALBANIDES and IMPLICATIONS for HYDROCARBON 

EXPLORATION 

D.A. Nieuwland 

NewTec International B.V. 

4e Binnenvestgracht 13 

2311NT Leiden, The Netherlands 

d.nieuwland@newtec.nl; dnieuw@xs4all.nl . 

This presentation integrates geo-mechanical aspects of thrust tectonics with analogue models 

and with observations on the Albanides and other natural examples. It will be demonstrated 

that understanding the mechanics of such a dynamic deformation process as thrust tectonics 

holds the key to generating a predictive model regarding the location of the prospective thrust 

front of the Albanides. At a smaller scale, the complex internal structure of the Albanides and 

the important fracture system are also largely governed by the geo-mechanical framework of 

the fold-and-thrust system. 

When studying a thrust tectonics system, it is good to realize that the mean stress of such a 

system is very high and that this has significant practical implications. This aspect is best 

illustrated with a Mohr circle diagram (Fig. 1). The Mohr circle example is constructed for a 

strong limestone at a reference depth of 1000 m. Note that the mode of failure of a strong 

Fig. 1. Formation of a thrust fault in a strong rock (e.g. cemented limestone) at a reference depth of 1000 m. 

121

ock in extension at the relatively shallow depth of 1000 m results in the formation of tension 

fractures (joints) and not in normal (shear) faults. Horizontal compression almost always 

results in the formation of shear fractures (faults). Thrust tectonics is the process of 

deformation by horizontal crustal shortening. The main compressive stress (!I) is horizontal, 

the intermediate stress (!II) is horizontal and parallel to the strike of the thrust faults the 

minimum stress (!III) is vertical. As a result the fault movements, in the (!I-!III) plain, are 

directed forwards and upwards. Thrusting is therefore often spectacularly expressed at the 

earth's surface by the formation of major topographic relief. The high mean stress is also 

expressed in high pore pressures in front of an advancing FTB and associated diagenetic 

effects in the foreland. Examples such as the Alps, Himalayas, Rocky Mountains, Zagros, the 

Andes and the Albanides speak for themselves. The Rocky Mountains, Zagros Mountains and 

the Andes all are known to contain major hydrocarbon accumulations. However, hydrocarbon 

exploration in fold-and-thrust (FTB) belts is not as mature as in extensional or strike-slip 

basins. One of the reasons is, that seismic in mountainous terrains is notoriously difficult to 

acquire and often of poor quality. In addition to the difficulties with acquisition and 

processing of the dominant exploration tool, the terrain and the structural geometries present 

an additional challenge for hydrocarbon explorers in FTB’s. Sandbox model examples are 

therefore very useful to assist seismic interpreters and geologists with conceptual models in 

their interpretation of the structural geometry and understanding of the kinematics of the 

complex FTB fault systems. 

Thrust belt deformation may involve basement (thick-skinned), or be limited to the 

sedimentary cover, which is detached from the basement (thin-skinned). Thrust faults form 

the outline of thrust sheets and are often associated with backthrusts. Backthrusts form as 

accommodation structures and do not have a detachment such as a full-scale thrust. Thrust 

sheets deform internally also by folding whereby two mechanisms can be recognized: - faultpropagation 

folding and fault-bend folding. On a smaller scale, calcite twinning and processes 

on atomic scale associated with dislocations in the crystal lattice can accommodate significant 

percentages of strain without the need for brittle failure. 

Ramp anticlines are fault-bend folds in the hanging-walls of thrust faults and are formed when 

thrust sheets are carried over flats and up ramps. The ramps are the actual thrust faults and 

most commonly have a dip of about 30 o . In uniform stratigraphy and without additional 

complicating factors, thrust faults form sequentially with regular thrust sheet lengths and 

spacing in normal-sequence from hinterland to foreland and characteristically form duplexes 

(Fig. 2). Complications such as syn-tectonic sedimentation or variations in basal friction cause 

out-of-sequence thrusting. Thrust faults may be separated by folds (soft-links), or by oblique 

or lateral ramps (hard-links), and when the separation becomes very large, by tear faults. 

Traps are often complex and relatively small, although some giant accumulations in thrusted 

anticlines are known (e.g. Cusiana, Colombia; Beykan, Turkey). Seismic imaging is 

commonly a problem, due to the structural complexity and mountainous terrains. In general 

one can use as a rule of thumb that basement involvement is most frequent in the hinterland 

(close to the indentor, creating the horizontal compression) and diminishes progressively in 

the direction of the foreland. Locally, pre-existing rift structures can complicate the 

geometries, they may be difficult to detect. Gravity modeling and palinspastic reconstruction 

are useful techniques to help solving problems of this nature. 

The nature of the detachment is of great influence on the geometry and kinematics of thrust 

structures. A low-friction decollement results in long thrust sheets with a straight front and 

many related backthrusts. A high-friction decollement results in short thrust sheets with a 

curved front and few or no backthrusts. Viscous or ductile non-viscous decollements such as 

respectively rock salt or clay, are both of a low-friction nature, but influence the thrust 

geometry in different ways. A change in basal friction from low to high has major 

122

consequences for the geometry and kinematics of a developing FTB. The Albanides are a 

good example of such effects and the implications for the overall geometry of the FTB and its 

consequences for hydrocarbon exploration. 

An analysis of the plate tectonic history of the Eastern Mediterranean, combined with a palaeo 

stress analysis provides the tectonic and geo-mechanical framework for the formation of the 

Fig. 2. 2D Seismic section E-W across the Albanides, showing anticlinal stacking and out-of-sequence 

deformation of thrusts and unconformities. 

Albanides. It will be demonstrated that the application of the regional analysis, integrated with 

the thrust mechanics provides the basics for the development of the exploration play concept 

for the Albanides and the Peri-Adriatic depression. 

The application of sandbox model analogue experiments is an additional tool that can be 

applied with significant practical consequences. This has been done so for the Albanides 

where the FTB front can not advance to within the Peri-Adriatic Depression due to a sudden 

increase in basal friction. The general applicability of small scale analogue models to large 

scale equivalents will be demonstrated with examples where analogue model results and 3D 

seismic data can be compared. In-situ stress measurements and detailed video-laser data 

acquisition in analogue experiments of thrust tectonics will provide further inside in the 

geometry and kinematics of FTB’s and on associated erosion and sedimentation processes. 

The punctuated equilibrium in the kinematics of a moving critical taper, as demonstrated with 

analogue model experiments, is expressed in maximum and minimum erosion and 

sedimentation periods, which are in turn expressed in the clastic sediments as turbidites in 

front of the advancing FTB. 

123

Fig. 3. In-situ stress measurements of the horizontal stress in a thrust tectonics analogue model experiment. 

S tress peak marks the formation of a thrust fault at the moment of break-through at the surface. 

Literature 

Jaeger, J.C & Cook, N.G.W., 1979. Fundamentals of rock mechanics. London, Chapman and 

Hall, 590 pp. ISBN 0-412-22010-5. 

Lacombe O. and Roure F., 2009. ‘From paleostresses to paleoburial in fold-thrust belts : 

preliminary results from calcite twin analysis in the Outer Albanides’. Tectonophysics, 

Special Issue on “Vertical movements, subsidence and uplift”. 

Mandl, G. 1988. Mechanics of tectonic faulting. Models and basic concept. Developments in 

Structural Geology 1, H. Zwart (Ed), Elsevier, 407 pp. 

Nieuwland D.A., Leutscher J.H. and Gast J.. 'Wedge equilibrium in fold-and-thrust belts. 

Prediction of out-of-sequence thrusting, based on sandbox experiments and natural examples'. 

Geologie en Mijnbouw 2000, v79/1, pp.81-91. 

Nieuwland D.A., Oudmayer B. and Valbona U.. 'The tectonic development of Albania: 

explanation end prediction of structural styles. Marine and Petroleum Geoscience, v18, pp. 

161-177, 2000. 

Nieuwland D.A., Urai J. and Knoop M.. 'In-situ stress measurements in model experiments of 

tectonic faulting.' Springer Verlag, 2000. In: Aspects of Tectonic Faulting'. Springer Verlag, 

1999. F.Lehner and J.Urai (Eds). 

Verschuren M., Nieuwland D.A. and Gast J.. 'Multiple detachment levels in thrust tectonics: 

sandbox experiments and palinspastic reconstruction.'. In: Buchanan P.G. & Nieuwland D.A. 

(Eds.) Modern developments in structural interpretation, validation and modelling', Geol. Soc. 

Special Publication No. 99, pp 202-227. 

124




The STRONGEST EARTHQUAKES OCCURRED in ALBANIA during 2009 

(M>5.0) and their SEISMOGENIC ZONES 

ORMENI Rr (1), DAJA Sh (2) and DODA V (1), 

(1) Institute of Geosciences, Polytechnic University, Tirana, “Don Bosko” street, Nr.60 

E-mail rrapo55@yahoo.com 

(2) Polytechnic University, Mining and Geology Faculty, Tirana, “Elbasani” street, 

Two of the strongest earthquakes in Albania during 2009 have occurred in Lezha-Ulqini and 

Lushnje-Elbasani-Dibra seismogenetic zones. First earthquake of magnitude (ML=5.0) and 

intensity (I0 = VI degree) occurred on August 21, 2009, in Adriatic Sea and second 

earthquake of September 6, 2009 (ML = 5.4) and intensity (I0 = VII degree), occurred in 

Gjorica, south of the city of Peshkopia, Albania. These earthquakes express the increased 

seismic activity during 2009 of the Lezha- Ulqini and Elbasan- Dibra seismogenetic zones. 

We present results from an analysis of local and regional data concerning epicenter location, 

focal mechanism of main shock and its aftershock activity. 

Composite focal mechanism of the main shock occurred on August 21 show a thrust fault: 

Strike=158°, Dip=50° and Rake (Slip)=90°. From the focal mechanism solution results that 

the earthquake of August 21, 2009 was triggered from a pure thrust fault with an NE-SW 

compression stress direction. The fault plane, has a dip 50° and has a trend NW-SE and is 

associated with the activation of the Ionian-Adriatic Sea deep fault zone of the earth crust at 

the border of the platform of the Adriatic Sea with orogen. The aftershock occurred 

northeastern of the main shock epicenter almost parallel of coastal line. The tectonic lines of 

Lezha-Ulqini seismogenic zone have served as structuring and discharge lines of seismic 

energy. In some cases where seismic energy flux failed to discharge through these lines, the 

process is accompanied by reverse faults, as is that of Ulqini area.. 

The focal mechanism of main shock occurred on September 6, has the parameters: strike 

219°, dip 40°, rake -90°, shows a normal active fault or fault zone with the extension axes in 

the NW SE direction. The aftershocks of main shock continued with a lower frequency as 

well as with lower magnitude values from September 9, 2009 and on. Mostly the foci of these 

secondary events are located in SW part of the epicenter zone, with a depth ranging from 1- 

29 km. This area is characterized by a complex geomorphology and in addition, has been hit 

by numerous earthquakes. 

During the last century some devastating earthquakes occurred in these seismic source zones, 

causing a great number of casualties and substantial damage. The epicenter of earthquake 

occurred on August 21, 2009 was situated on the Adriatic Sea 17 km West from Albania 

border and as a consequence has not damages. The earthquake occurred on September 6, 

2009 about 19 km south of the city of Peshkopia, caused more heavily damage in Gjorica, 

Qerenec villages and Shupenza municipality in Dibra district. The main event is a shallow 

one, with the hypocentral depth at 7.6 km. This fact explains the localized destruction in the 

epicentral zone. 

125

126




1D-VELOCITY MODELS and LATERAL CONTRASTS in ZONES DIVIDED 

by SHKODER-PEJA FAULT (ALBANIA) 

ORMENI Rr (1) and NAZAJ Sh (2) 

(1) Polytechnic University, Institute of Geosciences, Tirana, “Don Bosko” street Nr.60, 

rrapo55@yahoo.com 

(2) Polytechnic University, Mining and Geology Faculty, Tirana, “Elbasani” street, 

The Shkoder-Peja transversal deep fault of northeastern direction founded since the 

beginning of the Alpine cycle: during neotectonic stage, in the Pliocene-Quaternary, it 

was reconstructed with garben Gomsiqe-Puka-Iballa and Bajram Curri depression 

situated along it. This fault zone is potential transversal seismogenic belt in Albania and 

nearby. In the past centuries strong earthquakes have been generated at the extremities of 

this fault. In the future it is expected to generate strong earthquakes for the Shkoder-Peja 

deep fault of powerful structural reconstruction during the Pliocene-Quaternary. 

1D-velocity models of zones crosses by Shkodra-Peja deep transversal fault are 

computed at VELEST software of system SEISAN, inverting re- depths. The 

interpretation of the obtained 1D velocity models allows us to infer picked P-wave and Swave 

arrival time recorded in period of time 2002-2009 by the Albanian, Montenegro, 

and Macedonia seismic networks. Smooth velocity gradients with depth and low P-wave 

velocities are observed beneath two half-spaces crosses by Shkodra-Peja of the Albania 

Orogen. 

The lateral velocity difference in zones crosses this fault are as large as 2-6% and disturb 

in depth 0-30 km. The localizations based on 1D velocity models in presence of 2D or 3D 

velocity in homogeneities will be systematically shifted in the direction of increasing 

velocities. Since the difference increases with depth, the hypocenters are not only offset 

from the real fault but seem to mark even a slightly inclined fault, which is not the case. 

Precisely this is the cause for larger systematic misallocation and the determined fault to 

be deviated from the real fault. 

We defined reference velocity models for these zones for better constrain the hypocentral 

determination, in particular the hypocentral depths 

The interpretation of the obtained 1D velocity models and lateral velocity differences 

across Lushnje-Elbasan-Diber deep fault zones allows us to infer interesting features on 

the deep structure of the northen Albania. These results represent a first step towards 

more detailed Seismotectonic analyses. 

127

128




An INTEGRATED STUDY of the MØRE-TRØNDELAG FAULT COMPLEX, 

MID NORWAY 

Christophe PASCAL (1) , Aline SAINTOT (1) , A. NASUTI (1,2) , E. LUNDBERG (3) and C. 

JUHLIN (3) 

(1) 

NGU, Geological Survey of Norway (Christophe.pascal@ngu.no) 

(2) 

Department of Petroleum Engineering and Applied Geophysics, NTNU, Trondheim, 

Norway 

(3) 

Department of Earth Sciences, Uppsala University, Sweden 

The Møre-Trøndelag Fault Complex is one of the most prominent fault zones of Norway, 

onshore and offshore (Gabrielsen et al. 1999 and references therein). It strikes ENE-WSW, 

paralleling the coastline of south central Norway, and separates the northern North Sea basin 

system from the deep Mesozoic Møre and Vøring Basins. Onshore, the MTFC can be traced 

from the Møre region northeastwards along the northern margin of the Western Gneiss 

Region (WGR), and across the Grong–Olden Culmination towards the Børgefjell Basement 

Window, where it dies out in a horsetail splay (Fig. 1, Roberts 1998). 

Fig. 1: The Møre-Trøndelag Fault Complex as ENE-WSW topographic lineaments seen on a 

false colored RGB Landsat TM mosaic (band ratio R=5/4, G=3/1, B=5/7). 

During the Caledonian Orogeny, high ductile strain and the subsequent development of a 

steep ENE-WSW planar ductile fabric in the Precambrian high grade metamorphic (mostly 

129

gneissic) rocks occurred on the northern part of the WGR. The MTFC as discrete sinistral 

ENE-WSW steep ductile shear zones (Robinson, 1995) formed probably during the Scandian 

Orogeny towards the end of the Caledonian Cycle, since it slices through several of Scandian 

thrust sheets (Grønlie and Roberts 1989). The fault complex has been repeatedly reactivated 

in the brittle domain from Devonian time to the Cenozoic (?) and exhibits a great variety of 

fault rocks, exposed mostly on the Fosen Peninsula (i.e. Verran and Hitra-Snåsa faults, Watts 

2001 and references therein). These comprise mylonites overprinted by recrystallised breccias 

with quartz and epidote veining, phrenite-matrixed cataclasites, cut by zeolite/calcite veining 

associated with brecciation, pseudotachylites and zeolite-calcite slickenfibres. The complexity 

and variety of fault rocks reflects the longevity of the MTFC. The different fault rocks reveal 

the strength evolution of the fault complex and suggest significant weakening of some of its 

segments by repeated reactivation (see discussion in Pascal & Gabrielsen 2001). This applies 

to some of the primary segments of the present-day MTFC. Some segments of the southern 

onshore MTFC do not display such a cortege of fault rocks and exhibit, in turn, a restricted 

variety of fault rocks and associated mineralogy (Saintot & Pascal 2010). While epidote 

which might be the marker of the Devonian deformation, is widespread along the northern 

onshore segments of the MTFC, the southern segments are laumontite-rich and hence, are 

believed to represent the latest propagation (presumably Late Jurassic) and widening of the 

MTFC. 

Structural mapping in combination with analytical dating techniques have revealed three main 

phases of activity along the MTFC (Grønlie & Roberts 1989, Séranne 1992, Sherlock et al. 

2004): (1) Early Devonian sinistral strike-slip characterised by semi-ductile deformation, (2) 

Early Permian sinistral transtension and (3) Late Jurassic (to Early Cretaceous?) normal dipslip 

to dextral strike-slip. Normal dip-slip reactivation of the MTFC is assumed to have 

occurred in Cenozoic times (Redfield et al. 2005) but to date no clear evidence has been found 

yet. The three first phases of fault activity reflect, respectively (Gabrielsen et al. 1999): (1) the 

collapse of the Caledonian mountain chain, (2) widespread Permian rifting and (3) Late 

Jurassic rifting of the northern North Sea and the Mid-Norwegian margin. The MTFC appears 

to have exerted a strong influence on the evolution of the offshore basins, in particular in 

controlling their structural and depositional styles though time (Osmundsen et al. 2006). The 

fourth phase of activity of the fault complex was linked to the postulated uplift of the 

Norwegian mountains while the offshore basins were subsiding in Cenozoic times (Redfield 

et al. 2005). The MTFC appears to have strongly controlled the evolution of the landscape 

onshore, including the creation of preferential pathways for Quaternary glaciers. The MTFC 

is still seismically active today (Olesen et al. 2004). By means of numerical modelling, Pascal 

& Gabrielsen (2001) suggested that it acts as a very weak zone, resulting in disparate stress 

patterns to the north and south. Recent observations of stress-induced features and in-situ 

stress measurements support the modelling results (Roberts & Myrvang 2004). 

Little is known about the deep structure (e.g. dip directions of the faults), the links with the 

offshore fault segments and the precise kinematics and segmentation of the whole MTFC. The 

aims of the ongoing “MTFC integrated” project are (1) to reveal the deep structure of the 

MTFC using geophysical methods, (2) to investigate its offshore prolongation and (3) to study 

its kinematics and structural evolution. We use a large panel of geophysical methods, 

including gravimetry, magnetic profiling, shallow EM methods and seismic 

reflection/refraction profiles constrained by petrophysical sampling and structural 

observations. Our geophysical observations and experiments show that the MTFC onshore 

bounds a major horst structure similar to the ones evidenced by long-range seismic profiling 

offshore (Lundberg et al. 2009). Analysis of regional magnetic and gravity analysis allows for 

130

tracing the MTFC as curved system linking with the major detachments of the Møre Basin 

(Nasuti et al. 2010). 

In addition, fault slip analyses have been carried out on more than 200 fault planes. MTFCparallel 

slickensided planes developed along the ENE-WSW trending metamorphic foliation. 

The foliation was favourably dipping and orientated to be the locus of shear. Also we propose 

that the main fault segments which are deeply buried in the fjords dip strictly parallel to the 

foliation of the surrounding bedrocks. Normal kinematics and resulting extensional stress 

tensors are prominent. However, a non negligible amount of oblique normal slips along the 

parallel-to-foliation faults testifies for the strong control of the ductile planar fabric in the 

development of the faults and the accommodation of deformation. 

References 

Gabrielsen, R.H., Odinsen, T., & Grunnaleite, I., 1999. Structuring of the Northern Viking Graben 

and the Møre Basin; the influence of basement structural grain and the particular role of the Møre 

Trøndelag Fault Complex. Mar. & Pet. Geol., 16, 443–465. 

Grønlie, A., & Roberts, D., 1989. Resurgent strike–slip duple development along the Hitra–Snasa 

and Verran faults, Møre–Trøndelag fault zone, central Norway. J. Struct. Geol., 11, 295–305. 

Lundberg, E., Nasuti, A. & Juhlin, C., 2009. High resolution reflection seismic profiling over the 

Møre- Trøndelag Fault Complex, Norway. EGU 2009, Vienna. 

Nasuti, A., Ebbing, J., Pascal, C., Tønnesen, J.F. & Dalsegg E., 2010. Using Geophysical Methods 

to Characterize a Fault Zone – A Case Study from the Møre-Trøndelag Fault Complex, Mid- 

Norway. EAGE 2010, Barcelona. 

Olesen, O., et al., 2004. Neotectonic deformation in Norway and its implications: a review. 

Norwegian Journal of Geology, 84, 3-34. 

Osmundsen, P.T., et al., 2006. Kinematics of the Høybakken detachment zone and the Møre- 

Trøndelag Fault Complex, central Norway. J. Geol. Soc. London, 163, 303-318. 

Pascal, C., & Gabrielsen, R.H., 2001. Numerical modelling of Cenozoic stress patterns in the Mid 

Norwegian Margin and the northern North Sea, Tectonics, 20, 585-599. 

Redfield, T.F., et al., 2005. Late Mesozoic to Early Cenozoic components of vertical separation 

across the Møre–Trøndelag Fault Complex, Norway. Tectonophysics, 395, 233– 249. 

Roberts, D., 1998. high-strain zones from meso- to macro-scale at different structural levels, Central 

Norwegian Caledonides. J. Struct. Geol., 20, 111-119. 

Roberts, D., & Myrvang, A. 2004. Contemporary stress orientation features and horizontal stress in 

bedrock, Trøndelag, central Norway. NGU Bulletin 442, 53-63. 

Robinson, P., 1995. Extension of Trollheimen tectono-stratigraphic sequence in deep synclines near 

Molde and Brattvåg, Western Gneiss Region, southern Norway. Norwegian Journal of Geology 75, 

181-198. 

Saintot, A. & Pascal, C., 2010. A contribution to the kinematics of the Møre-Trøndelag Fault 

Complex (Western Norway). EGU 2010, Vienna. 

Sherlock, S.C., et al., 2004. Dating fault reactivation by Ar/Ar laserprobe; an alternative view of 

apparently cogenetic mylonite-pseudotachylite assemblages. J. Geol. Soc. London, 161, 335-338. 

Séranne, M., 1992. Late Paleozoic kinematics of the Møre-Trøndelag Fault Zone: and adjacent areas, 

Central Norway. NGT, 72, 141-158. 

Watts, L.M., 2001. The Walls boundary Fault Zone and the Møre-Trøndelag Fault complex: a case 

study of two reactivated fault zones. Unpublished PhD thesis, University of Durham, U.K., 550 pp. 

131

132




STRATIGRAPHIC CORRELATION of RADIOLARIAN CHERTS BELONGING to 

the OPHIOLITE-BEARING and the CARBONATIC SUCCESSIONS 

Mensi PRELA 

(oral presentation) 

Polytechnic University of Tirana; Faculty of Geology and Mining, Earth Sciences Department 

The Jurassic radiolarian cherts of Albania are included both in the ophiolitic successions of 

the Mirdita zone (Kalur Cherts), which have been interpreted as remains of the Tethyan 

oceanic lithosphere, and in carbonate successions presumably deposited on the continental 

margin of the Tethys. 

The data available on the radiolarian cherts of Albania are summarized and updated in this 

paper. The data from 12 sections of radiolarian cherts belonging to the ophiolite-bearing 

successions are examined and compared with data from 14 sections of radiolarian cherts 

belonging to the carbonate (pelagic and paltformic) successions. 

Stratigraphical data of the top of the ophiolite sequence and of the carbonate peripheral units 

indicate their similar paleogeographical conditions and close relations between them. 

133

134




The AGE of the RADIOLARIAN CHERTS in the WESTERN CARBONATE 

PERIPHERAL UNITS of the ALBANIAN OPHIOLITES 

Mensi PRELA 

(poster presentation) 

Polytechnic University of Tirana; Faculty of Geology and Mining, Earth Sciences Department 

In this paper we examined radiolarian assemblages in six sections of chert levels intercalated 

in carbonate successions of the Mesozoic Albanide continental margin: Porava, Karma, 

Shushica, Derstila, Vithkuqi and Barmashi. 

In Shushica, Karma, Barmashi and Vithkuqi sections radiolarian cherts rest directly on the 

platformal thick-bedded, stromatolitic limestones, or on the condensed nodular limestones 

laying above the stromatolitic limestones. In Porava and Derstila sections radiolarian cherts 

rest on the cherty limestones. 

The age of the radiolarian cherts in examinated sections can be related to Middle Jurassic. 

The ages of the radiolarian assemblages determined in the cherts of the carbonate successions 

are the following: 

Porava - Latest Bajocian-Early Bathonian to Middle Bathonian (5-6 UAZ) 

Karma – Early Bajocian to Latest Bajocian-Early Bathonian (4-5 UAZ) 

Shushica - Latest Bajocian-Early Bathonian (5 UAZ) 

Derstila – Latest Bajocian-Early Bathonian to Middle Bathonian (5-6 UAZ) 

Vithkuqi – Middle Bathonian (UAZ 6) 

Barmashi - Latest Bajocian-Early Bathonian (5 UAZ) 

135

136




HYDROCARBON OCCURRENCES and PETROLEUM GEOCHEMISTRY of 

ALBANIAN OILS 

Irakli PRIFTI and Kristaq MUSKA 

(Polytechnic University of Tirana) 

A wide range of geochemical data from Albanian oils have been collected, documented and 

reviewed. 

Oil generation has occurred in two phases, first during an Early Miocene phase when the 

source rocks were in early stage to main part of the oil maturity window, and later during the 

Pliocene, when the advanced stage of oil generation was reached. The multi-phase generation 

has resulted in hydrocarbon accumulations with a wide range of geochemical 

characteristics. In individual fields or field complexes, heavy oils, both biodegraded and 

non-biodegraded, light oils, condensates, wet and dry gas may occur. In general, oil density 

sulphur content decrease with depth. 

Oil groupings are evident from the data set, although stable carbon isotope values suggest that 

the oils from the Berat Belt and the oils from the Preadriatic Depression could be separated 

from the majority of oils in the Kurvaleshi Belt. No correlations between oils and individual 

carbonate source rock levels could be established. 

The Tertiary humic source rock is probably early mature, and has generated dry gas and 

some condensate. The gas accumulations in the Preadriatic Depression contain mostly 

biogenic gas and mixed thermogenic/biogenic gas. The deeper clastic reservoirs contain 

relatively less dry gas, and less non-hydrocarbon gas. 

GEOLOGICAL FRAMEWORK 

The geology of the Albanides is characterized by complex structural features resulting from 

westward overthrusting, Appendix A: Geologic Section A-A' west to east in northern Albania 

and Geologic Section B-B' north-northwest to south southeast through oil fields in central 

Albania with major stratigraphic units illustrated. The geological and tectonic frameworks are 

similar to the Italian Adriatic province (Curi, F. t 1993). The geologic setting of Albania can 

be broadly divided into the thrust belt(s), the foredeep, and the foreland domains. The 

Albanian study area consists of the Pre-Adriatic Depression and three external Albanide 

geotectonic zones: (from west to east) Sazani, Ionian, and Kruja, Map 1. In Greece, the three 

geotectonic zones, Pre-Apulian, Ionian, and Gavrovo, occur in front of the major westdirected 

Pindus thrust fault and have been defined oa the basis of different sedimentary facies 

of exposed Mesozoic: and Cenozoic rocks and on different tectonic styles. The current 

structure of the External Albanides is a result of the collision of the Adria continental margin 

with the European plate. 

The Albanian thrust belt includes the Krasta (a fourth and easternmost zone), Kruja, and 

137

Ionian zones. The thrust belt is characterized by successive folds of the ancestral Ionian basin 

sediments that have been thrust westward. The Krasta zone's most important compressional 

tectonic phase took place during Late Eocene while Kruja zone thrusting occurred during 

Middle Oligocene and Ionian zone thrusting occurred during the Middle Miocene. The Ionian 

Zone's Berati Belt underwent compression during Upper Oligocene-Lowermost Miocene 

(Aquitanian) whereas the Kurveleshi and Cika Belts were thrust-folded at the end of the Lower 

Miocene. 

The geology of each hydrocarbon bearing zone is discussed in more detail below. The 

sediment Ethologies for the Pre-Adriatic Depression and the External Albanide zones are 

summarized in Appendix B: Stratigraphic Columns for the External Albanides and the Pre- 

Adriatic Depression. 

W 

Patos-Marinza oilfields 

HYDROCARBON OCCURRENCES 

Figure 1: Oilfields from Patos-Marinza and Kuçova. 

Kuçova oilfield 

Many oil and gas accumulations, asphalt veins, oil-stained rocks, and gas seeps exist in 

Albania. They are part of a broader belt of scattered hydrocarbon fields and seepages on both 

sides of the Adriatic Sea and the Ionian Sea. 

In Albania, the oil discoveries are concentrated in the thrust belt's Ionian Zone and in the Pre- 

Adriatic Depression. Within the Ionian Zone most of the commercial oil fields occur in the 

Kurveleshi Belt. 

The Marinza oil field is the largest producing field in Albania. Marinza has several productive 

beds for every reservoir suite. The reservoirs are Tortonian and Messinian sandstones that 

overlie thrust anticlines of eroded limestones at the Intra-Miocen Unconformity. The oil 

migrates from limestone reservoirs into sands and sandstones in the oil fields of the Pre- 

Adriatic Depression. The formation water salinities in sandstone deposits are typically 

between 20 g/L and 30 g/L (20,000-30,000 ppm) and decrease with depth. Thus, meteoric 

water may be moving through the deposits. The average salinities in fields with carbonate 

reservoirs are between 40 g/L and 70 g/L (40,000-70,000 ppm). 

The largest oil accumulation in limestone reservoirs occurs in the Cakran field. Cakran is 

estimated to have 1000 m of structural closure of condensate and light oil pay (49° API). The 

limestone oil fields of Albania have normal pressures and typically low reservoir 

temperatures (35°C to 94°C with the highest being in the exceptional Vlora structure and 

measured at 4550m). The geothermal gradient in Albania is usually very low at 1.6°C/100m. 

In oil fields with limestone reservoirs, non-hydrocarbon gases comprise 1.8% to 15.0% of the 

138 

E

gas with hydrogen sulfide concentrations that range from 0.5% to 10.0% of the total gas. Three 

oil field trends exist in the Kurveleshi Belt in the central part of the Ionian Zone(figure 2): 

Figure 2. Albanian oil fields in limestones section 

139

1. In the west: Amonice-Gernec-Gorsht/Kocul. 

2. In the center: Mollas-Cakran-Kreshpan. 

3. In the east: Karbunare-Hekali-Ballshi-Visoke-Sheqishte-Kallm/Verri/Kolonje. 

Additional Kurveleshi Belt hydrocarbon accumulations that occur in the southern part of 

Albania include Delvina (condensate) and Finiq-Krane (gas and oil). 

Commercial oil fields have been discovered in the Pre-Adriatic Depression. Oil fields include 

the Patos/Marinza/Bubullima/Kolonje complex, the Pekisht/Rasa/Murizi complex- and 

Kuçova. 

PETROLEUM GEOCHEMETRY RESULTS and DISCUSSION 

Many crude oils, oil show extracted liquids, and oil seep samples representative of all 

major Albanian oils have been selected for geochemical characterization. The samples are 

identified by their respective well (or outcrop location), field, producing interval, reservoir 

lithology, geographic/geologic zone and zone belt. 

Geochemical results will be discussed in the following order: oil characterizations and oil 

grouping. 

CRUDE OIL PROPERTIES 

Bulk crude oil properties, chemical compositions, stable carbon isotopic compositions, 

and selected isoprenoid and n-paraffin parameters (e.g., Pristane/Phytane, Pristane/nC17, 

Phytane/nC 18) 

from whole oil gas chromatograms (GC). Oil characteristics vary broadly 

for Albania's production oils. API gravities range from 57° API to 10° API (densities 

from 0.75 to 1.0 g/mL). The current properties reflect the combined effects of the 

respective source rock kerogen characteristics, source rock thermal maturities at the time 

of hydrocarbon expulsion, and local bacterial degradation/water washing. 

BlODEGRADATION 

The heavy oils and moderately heavy oils from Kreshpani-3 (10.7°API; S=4.9%), 

Bubullima-42 (12.5°API; S=5.6%), Ferma-30 (18.5°API; S=4.3%), and Rasa-8 

(21.1°API; S=3.8%) show no sign of biodegradation, and their moderately high benzene 

and toluene contents indicate water washing effects are minimal, (whole oil gas 

chromatograms). A number of oils in Albania contain moderately high concentrations of 

sulfur. A correlation exists between higher sulfur concentrations and lower API gravities 

and Figure 3 illustrates Albanian oil data. 

Biodegradation has affected several oil accumulations in Albania (e.g., from wells Drashovica- 

33, Vlora-10 oil show, Ballshi-55, Gorisht-77, Marinza-1850, Vurgu-7, Arza-16, Patos -1449, 

Kozare-568, Kreshpani-4, Panaja-10, Povelca-lB, and the Kuçova seep) and has probably 

lowered the API gravities from their intrinsic values; but the respective kerogen chemical 

compositions remain the principal control of final oil gravities. For heavy, high sulfur, 

biodegradation causes minimal changes in API gravities and total sulfur contents because the 

original n-paraffin contents are a low percentage of the crude oil. 

140

GROUPING of ALBANIAN OILS 

Oils from Albanides are grouped on the basis of the geochemical properties, geographical and 

geological location. According to their properties are divided six families oils and subgroups 

within them: 

1. First family met in the gas fields, appears in the form of condensates, and is immature. 

Their origin is related to the resinites derived from terrestrial plants. 

2. The second family includes oils from Tirana- Ishmi depression, are met from shallow wells. 

Isotopic ratio is higher and his value fluctuates around -22 0 / 000. 

3. The third family, represented by the oil meeting in the southern Ionian area. In this family 

includes oils from wells; Prishta-14, Vurgu-7 and condensates from Delvina. Characterized by 

the stable carbon isotopic ratio that fluctuates around -26 0 / 000 and predominate diasterane to 

sterane (Delvina, Vurgu-7). In this family shared three subgroups oils: 

1.Delv.-4, Delv.-12; 

2. Prishta-1; 

3. Vurgu-7; 

141

4. A family of four, including all Albanian oils, the stable carbon isotopic ratio fluctuate in 

value -27 0 / 000 ÷ -29 0 / 000 and Diasteranes/Regular sterane is lower, with the exception of oil that 

we get the well-Kreshpan 3. This family includes six subgroups oil: 

1. Amon-16,Gor-77, Ballsh-55, Patos-1449,Vis-177,Hek-10,Hek-12; 

2. Cakran-18,Cakran-47; 

3. Marinza-952,1850; Bub-42; 

4. Kolonja-691, Kreshpan-3; 

5. Kozara-568, Rasa-8, Arza-16, Ferma-30; 

6. Drashovic-33, Vlora-11, Kreshpan-4. 

Subgroup oil "5" distinguished from others as are generated by source rocks with high content of 

clay fraction. 

5. The fifth family includes oil well received in Vlora-10 and signs of oil meeting in the salt 

mine in Dhrovjan. Raporti isotopik i karbonit ne fraksionin aromatik dhe metano-naftenik 

luhatet ne vlera te ulta -29.5 0/000 ÷ -32 0/000 . the stable carbon isotopic ratio in aromatics 

and saturates hydrocarbon fluctuate in value -29.5 0 / 000 ÷ -32 0 / 000. 

6. Family of six oil represented only in well get Zvernec-3. Oil might be the rare honor since 

its composition Diasteranes missing. 

CONCLUSION 

In Albania, oilfields are concentrated in the thrust belt's Ionian Zone and in the Pre-Adriatic 

Depression. Within the Ionian Zone most of the commercial oil fields occur in the Kurveleshi 

Belt within limestone section. While oilfields from Pre-Adriatic Depression occur in 

142

sandstones of Miocene deposits. 

Albanian crude oils are included in different thermal maturities, some with higher thermal 

maturities tend to have higher API gravities if all other factors are the same. However, other 

causal factors clearly play important roles. For example, API gravities are about the same for 

the oils from the Marinza-952 well, the Prishta-1 well, and the Vlora-11 well (API - 32-9°, 

33.5°, and 30.4°, respectively); however, their thermal maturities range from the main phase of 

oil generation to advanced oil window maturity. The thermal maturity of the Kreshpani-3 well's 

oil is virtually identical to the maturity of the Prishta-1 well's oil, but the sulfur contents are 

very different (S - 4.89% and 0.99%, respectively). These five oils are not biodegraded so the 

principal control on their API gravities or total sulfur contents is the type of kerogen in their 

source rocks. Their thermal histories are a secondary control of the final gravities and sulfur 

contents. 

Post-accumulation factors such as biodegradation can alter the oils to give somewhat lower API 

gravities and slightly higher sulfur contents by removing the n–paraffin hydrocarbons and low 

molecular weight components. Once again, the type of kerogen in the oils' respective source 

rocks is the principal causal factor in the resultant oils' API gravity and sulfur content, but 

biodegradation is a secondary factor determining the final bulk oil properties. 

These phenomena cause partition in six families of oils. 

REFERENCES 

PRIFTI I. and MUSKA K. 1999. Identification of oil accumulations in Miocene deposits by 

geochemical parameters. In: 19th International Meeting on Organic Geochemistry,Istanbul 

/ Turkey , September 1999. 

VELAJ T and PRIFTI I. 1996. On hydrocarbon potential in Albania. In: 2nd International 

Symposium on the Petroleum Geology and Hydrocarbon Potential of the Black Sea Area. 

Sile Istanbul,Turkey, September 1996. 

PRIFTI I. and MUSKA K. 2003. Classification of Albanian oils. In: Scientific meeting 

“Albanian geology in time”, (From Franc Nopça ). Tirane, November 2003. 

143

144




MINERALOGICAL and PETROLOGICAL CHARACTERISTICS of SHALLOW MARINE 

FORMATION in BRARI SECTION, ALBANIA 

Ana QORRI* 

(Poster) 

*Polytechnic University of Tirana, Faculty of Geology and Mining, Department of Earth Sciences. 

anaqorri@gmail.com 

Brari is located in Tirana Depression, which is situated in the north-eastern side of Periadriatic 

Depression. The Brari section belongs to inner-outer and outer neritic zones. Marine sediments of 

Brari section consist of basal sandy conglomerate beds with concretions, yellowish calcareous 

sandstones, cross bedded conglomerates and very thin layers of silty mudstones, parallel bed 

gravelites, massive fossiliferous sandstones with bivalves. Upward the section continues with 

Lithothamnium limestones. terrigenous succession and again Lithothamnium limestones. XRD and 

SEM analyses indicate that quartz, calcite, dolomite, mica, feldspars minerals are dominant in this 

study area. Those are extremely weathered. The presence of chlorite, smectite was carried out by 

the XRD analyses, after several treatments of the samples. 

Keywords: Brari section, XRD (X-Ray Diffractometry), SEM-EDS (Scanning Electron 

Microcopy- Energy Dispersive Spectroscopy), Clay minerals. 

1- INTRODUCTION and OBJECTIVES. 

Brari is located in the south-eastern part of 

Tirana Depression. Brari section was 

measured and sampled in 1999, during a field 

trip, by the members of a project ( Meço, 

145 

Durmishi, Gjani, Kleinholter). Aquitanian, 

Langhian, Serravallian, Tortonian successions 

are determined into this section (Fig.1). The 

Serravallian- Tortonian deposits show marine 

conditions.

The primary purpose of this study is to 

determine the textural and mineralogical 

characteristics of this Neogene unit in respect 

to their genetic relationship. The second is to 

determine the principal minerals in the study 

area. The third and the most important is to 

identify the clay minerals, and to give a full 

description of them. Realizing all of this 

objectives, can give to us a useful and an 

exact information of the forming history of 

the sediments this area. 

2- METHODS of STUDY. 

Fig.1 Geological Map of Tirana Depression (According to the Geological 

Map of Albania. 1:200 000). 

In this study 11 clay samples were collected 

from the bottom to the top of the section. The 

mineralogical characteristics of the samples 

were determined through several techniques, 

including XRD and SEM-EDS methods. For 

petrographic studies and electron microscopy 

9 normal thin sections were prepared from the 

most characteristic samples. The mineralogical 

composition of the samples was 

examined using X-Ray Diffraction under 

CoK� radiation, with a step scanning 3 to 

60º2� in steps of 0.01º2� with a counting time 

of 1.00 s per step. First X-ray Diffraction 

Analyses were done from the samples in natural 

conditions and after this were selected the 2 most 

representative samples. The analyses aimed at 

documenting the gross mineralogy, and specially 

clay mineralogy of Brari Section. A clay fraction 

(< 2 µm) was separated out from the samples by 

disaggregating with different acids according to 

Jackson Method and dispersing the sample in 

distilled water and immediately washed by 

centrifugation. The fraction of < 2 µm was 

isolated by centrifugation and suspension were 

dried on glass slides. The clay samples in oriented 

mounts were run under three separate conditions: 

1) air dry state. 

2) after heating to 550º C for 2 hours and 

3) after ethylene glycol treatment 

3- RESULTS and DISCUSSION. X-ray diffraction 

146 

Brari 

The digital data were interpreted using X-Pert 

Highscore Plus software, which comprises a 

search-match routine based on a Powder 

Diffraction File.

Minerals identification by XRD indicated that 

the main minerals are quartz, feldspar, mica 

chlorite, smectite (after the treatment of the 

samples) and a small quantity of serpentine. 

However, minor amount of feldspar is still 

SEM-EDS 

present in many of the samples (Fig.2), and 

trace amounts of calcite and dolomite are also 

present in many samples(before the treatment 

of the samples with the acids). 

As a confirmation of XRD analyses even 

under SEM the minerals identified in thin 

sections are: quartz, as the main constituent, 

dolomite in form of cement, feldspar 

weathered into clay minerals (chlorite), 

Fig.2 XRD pattern of sample Alb_34 B/22/1 from the study area. 

Fig.3 Several minerals identified at thin section no. 

Alb_66_01. Q- Quartz; M-Muscovite; Fsp-Feldspars; 

Do-Dolomite; I-Ilmenite; R-Rutile; Zr-Zircon 

147 

biotite elongated like flakes, white dots of 

pyrite, muscovite is also present (Fig.4), in its 

composition has a considerable quantity of 

Mg and Ca, because of dolomite cement. To 

notice is the presence of many minerals which 

are accessory minerals in igneous rocks, like 

ilmenite, monazite, zircon (Fig.3) etc. 

Conclusion 

Fig.4 EDS spectrum for muscovite.

Non Clay Minerals present in Brari section 

are: 

Quartz: Quartz forms one of the most 

abundant minerals in most of the samples. 

Quartz is identified by its distinctive 

reflections at 4.26 Å and 3.35 Å. The 3.35 Å 

peak of quartz was more intense than the 

other peaks. There was a coinciding in some 

samples, with a strong reflection of illite at 

3.33 Å which makes this 3.35 Å peak difficult 

to use, due to as quartz is abundance. 

Feldspar: Feldspar is the next important nonclay 

mineral present in most of the samples 

but in minor amount. It is identified by 

distinct reflection in the spacing range of 3.8 

Å to 3.2 Å 

Calcite: Calcite is identified by only a weak 

reflection at 3.01 Å showing its presence in 

trace amounts. 

Dolomite: Dolomite is identified by only a 

weak reflection at 2.8 Å, indicating a trace 

amount of the mineral. 

Muscovite: Muscovite is identified by not 

such a strong reflection at 10.1 Å, indicating 

his presence in our samples. 

Clay Minerals present in Brari section are: 

Chlorite: Chlorite is represented by its basal 

reflections at 14.25 Å, 7 Å, 4.7 Å and 3.5 Å 

respectively. The basal reflection at 14.25 Å 

could not be used directly for the 

identification of chlorite because of an 

interfluence with an Illite-Smectite mixed 

layer, and 7.14 Å also could not be used for 

chlorite identification because of the 

interference and coincidence of kaolinite 

reflections. 

Smectite: Smectite was identified using XRD 

technique. The petrographic and mineralogycal 

studies indicate that smectite is the earliest 

mineral to form due to the transformation 

reactions. 

148 

ACKNOLEDGEMENTS 

The author is grateful to Prof.C.Durmishi for 

creating the possibility to take this samples in 

Poland. Many thanks are due to Prof. Eleni 

Gjani and to the professors of the Faculty of 

Earth Sciences, Sosnowiec, Poland, for their 

help with the SEM and XRD analysis. 

BIBLOGRAPHY 

E.Gjani, S.Meco, F.Strauch (2003) -Litho- 

Biostratigraphic data on the Tirana 

Depression(Albania) and their correlation 

with the Periadriatic Depression. pp.723-736. 

E.Neczko (1965), - Clay Minerals, pp.329- 

354. 

W. S. Mackenzie, C. H. Donaldson, C. 

Guilford – Atlas of Igneous Rocks and Their 

Textures (1982) 

W. S. Mackenzie, Adams, C. Guilford– Atlas 

of Sedimentary Rocks Under the Microscope 

(1981) 

W. S. Mackenzie, C. Guilford– Atlas of Rock- 

Forming minerals in this section (1978) 

K. Ibrahim - Mineralogy and chemistry of 

natrolite from Jordan (2003) 39, 47–55.




ACTIVE BASINS and NEOTECTONICS: MORPHOTECTONICS of the LAKE 

OHRID BASIN (FYROM and ALBANIA) 

Klaus REICHERTER 1 , Katja LINDHORST 2 , Nadine HOFFMANN 1 , Sebastian 

KRASTEL-GUDEGAST 2 , Ariane LIERMANN 1,3 and Ulrich A. GLASMACHER 3 

1 

Institute of Neotectonics and Natural Hazards, RWTH Aachen University, Lochnerstr. 4-20, 

52056 Aachen, Germany 

2 

IFM-Geomar, Kiel, Germany 

3 

Institute of Earth Sciences, Research Group: Thermochronology and Archaeometry, 

University Heidelberg, Im Neuenheimer Feld 234 69120 Heidelberg, Germany 

Corresponding author: K. Reicherter, mail: k.reicherter@nug.rwth-aachen.de 

The Lake Ohrid Basin in the extensional part of FYROM (Former Yugoslav Republic of 

Macedonia) and Albania meets all criteria of an active, seismogenic landscape: linear steplike 

fault scarps in the landscape and under water within the lake. The neotectonic and 

landscape evolution of the southern Albanian fold-and-thrust belt and the Albanian-FYROM 

extensional back-arc area (basin and range type) are directly linked to subduction and 

subduction roll-back within the Hellenic trench system (Fig. 1). The initiation of the Ohrid 

Basin is estimated between 2 and 8 million years. 

Figure 1: Structural cross section from the Adrian coast to the Neogene basins in the 

Balkanides. Within the extensional domain basins form, whereas the frontal part is 

characterised by thrusts. 

149

The deformation can be divided in three major deformation phases (1) NW-SE shortening 

from Late Cretaceous to Miocene with compression, thrusting and uplift; (2) uplift and 

diminishing compression during Messinian - Pliocene; (3) vertical uplift and (N)E-(S)W 

extension from Pliocene to recent associated with (half-) graben formation. This latter phase 

of an orogenic collapse is related with a seismogenic landscape with linear step-like fault 

scarps on land and offshore. 

Figure 2: Morphotectonic features of the Lake Ohrid Basin from SW. O = Mirdita ophiolites 

(Jurassic-Cretaceous), C = Carbonates (Triassic), M = Molasse (Tertiary), p = polje. 

A tectonic multi-proxy approach (palaeostress analysis, geophysical and remote sensing 

methods) has been made to reveal the stress history, the neotectonic history and tectonic 

geomorphology of the Lake Ohrid region. Post-glacial (or Late Pleistocene) bedrock fault 

scarps at Lake Ohrid are long-lived expressions of repeated surface faulting in tectonically 

active regions, where erosion cannot outpace the fault slip. Other morphotectonic features are 

wind gaps, wineglass-shaped valleys and triangular facets, which are well preserved. 

Generally, the faults and fault scarps are getting progressively younger towards the basin 

center, as depicted on seismic and hydroacoustic profiles. The geomorphology also points to 

rotated and tilted blocks. Additionally, mass movement bodies within the lake and also 

onshore (rockfalls, landslides, sub-aquatic slides, homogenites, turbidites) are likely to have 

been seismically triggered. These morphotectonic observations are in line with focal 

mechanisms of earthquakes in the greater Lake Ohrid area. 

Furthermore, apatite fission-track (A-FT) analysis and t-T-paths modelling was performed to 

constrain the thermal history, and the exhumation rates. For fission-track analysis apatites 

were separated from a suite of granitoid rocks from basement units and from flysch- and 

molasse-type deposits of Paleogene to Neogene age. Apatites show a range of the apparent 

ages from 56.5±3.1 to 10.5±0.9 Ma. The spatial distribution of ages suggests different blocks 

with a variable exhumation and rock uplift history. Fission-track ages from molasse and 

flysch sediments of the basin fillings show distinctly younger ages. Generally, the Prespa 

Basin reveals A-FT-ages around 10 Ma close to normal faults, whereas modelling results of 

the Ohrid Basin suggest a rapid uplift initiated around 1.4 Ma associated with uplift rates (? 

rock uplift rates or surface uplift rates?) on the order of 1 mm/a. As a conclusion we observe a 

150

westward migration of the extensional basin formation, i.e. the initiation of the Prespa Basin 

occurred well before the formation of the Ohrid Basin. 

Figure 3: Sketch of the major neotectonic features at Lake Ohrid resembling a “seismogenic” 

or “paleoseismic” landscape. Note the Kosel hydrothermal field along a major fault in 

the north. The earthquake zone brackets the focal depth of instrumentally recorded 

earthquakes in the area, which is between 12 and 25 km depth. 

References 

Hoffmann, N., Reicherter, K., Fernández-Steeger, T. and Grützner, C. (2010, accepted): 

Evolution of ancient Lake Ohrid. A tectonic perspective. Biogeosciences, Special Issue: 

Evolutionary and geological history of Balkan lakes Ohrid and Prespa. 

Wagner B., Reicherter, B., Daut, G., Wessels, M., Matzinger, A., Schwalb, A., Spirkovski, Z. 

and Sanxhaku, M. (2008): The potential of Lake Ohrid for long-term 

palaeoenvironmental reconstructions. Palaeogeography, Palaeocology, 

Palaeoclimatology, 259, 241-356. 

151

152




KINEMATIC and PETROLEUM MODELLING in the ALBANIDES 

François ROURE* , **, Laurie BARRIER* , ***, Jean-Paul CALLOT*, Kristaq 

MUSKA**** and Nadège VILASI* , ***** 

*IFP Energies Nouvelles, 1-4 Avenue de Bois Préau, 92852 Rueil-Malmaison Cedex, France 

**VU-Amsterdam, de Boelelaan 1085, 1081HV Amsterdam, the Netherlands 

***current position, IPG-Paris 

****Polytechnic University, Tirana 

*****current position, Statoil 

corresponding author: Francois.ROURE@ifpenergiesnouvelles.fr 

Basin modelling tools are now more efficient to reconstruct palinspastic structural cross 

sections and compute the history of temperature, pore fluid pressure and fluid flow 

circulations in complex structural settings. 

For instance, IFP Energies Nouvelles has developed since a couple of years numerical tools 

such as Thrustpack, Dionisos and Ceres, aiming at forward kinematic modelling, stratigraphic 

modelling, as well as fluid flow, pore fluid pressure and HC generation and migration 

modelling. These tolls have been integrated here in a specific workflow dedicated to a better 

assessment of the petroleum systems in the tectonically complex Albanides thrust belt. 

Regional seismic profiles have been first interpreted and calibrated against exploration wells. 

Resulting interpretations have been depth converted. Three parallel structural sections have 

been then balanced and unfolded, the resulting initial geometries being used as an input data 

to initiate the forward Thrustpack modelling. For each incremental stage of the deformation, 

Dionisos was used to simulate the deposition pattern of the synorogenic sediments, starting 

from the Oligocene flexural flysch sequence until the last Plio-Quaternary stages of 

deformation, including numerous incremental Miocene thrust episodes. 

Ultimately, Ceres modelling was also applied to one of these Albanian sections, using the 

result intermediate geometries obtained during the Thrustpack modelling as geometric targets 

to calibrate intermediate stages in Ceres. 

The results of this fluid flow and petroleum modelling are finally discussed with respect to the 

known petroleum occurrences in the Albanides and the adjacent Adriatic foreland. 

More details on the coupling between Thrustpack and Dionisos softwares and on the Ceres 

modelling will be presented in two companion posters, i.e. Barrier et al. and Vilasi et al. 

153

154




ALPINE INVERSION of the NORTH AFRICAN MARGIN and DELAMINATION of 

its CONTINENTAL LITHOSPHERE 

François ROURE* , **, Piero CASERO***, and Belkacem ADDOUM**** 

*IFP Energies Nouvelles, 1-4 Avenue de Bois Préau, 92852 Rueil-Malmaison Cedex, France 

**VU-Amsterdam, de Boelelaan 1085, 1081HV Amsterdam, the Netherlands 

***Roma, Italy 

****Sonatrach, Division Exploration, Avenue du 1° Novembre, BP68M, Boumerdes 35000, 

Algeria 

corresponding author: Francois.ROURE@ifpenergiesnouvelles.fr 

The former Mesozoic passive margin of North Africa has been strongly influenced by the 

Cretaceous to Neogene Alpine deformations, making difficult to trace its initial contours 

between the Saharan Atlas and Apulia in the west, and its current extent and architecture 

beneath the allochthon of the Ionian-Calabrian arc and adjacent Mediterranean Ridge in the 

east. 

A rim of Tethyan ophiolitic sutures can be traced more or less continuously from Turkey and 

Cyprus in the east, in onshore Crete, in the Pindos in Greece and Mirdita in Albania, as well 

as in the Western Alps, Corsica and the Southern Apennines in the west, implying that both 

the Apulia/Adriatic domain and the Eastern Mediterranean Basin belong to the southern 

margin of the Tethys. Because there is no evidence of vertical offset of the Moho beneath the 

Mediterranean arcs, we propose to apply a new model of delamination of the continental 

lithosphere, recently documented in the southeastern Carpathians, to the Apennines and the 

Aegean, where the paleo-oceanic suture is indeed exposed in the hinterland. According to this 

model, only the mantle lithosphere of Apulia and the Eastern Mediterranean has been and is 

still locally subducted and recycled in the asthenosphere, the northern portion of the African 

crust and coeval Moho being currently decoupled from its former, currently delaminated and 

subducted mantle lithosphere. 

Although the Kabylides and Peloritan units have been for a long time assumed to be of 

European affinities, there is no evidence of any ophiolitic suture in Algeria, Tunisia nor Sicily 

between the stable African foreland and these far-travelled accreted terranes. Therefore, the 

former substratum of the Tellian units still remains conjectural, this intervening domain being 

either related to a truly oceanic or instead to a formerly thinned but still continental 

lithosphere. 

Accurate dating of the synflexural and synkinematic series helps to trace the spatial and 

temporal evolution of the regional foreland flexure developing in front of advancing nappes, 

and which indeed records the effects of thrust loading and slab pull. Synorogenic sediments 

help also to precise the timing of thin-skinned deformation, which occurred mainly prior to 

the Upper Miocene in Algeria, but was still active during the Pliocene and even the 

Quaternary in the Southern Apennines and along the eastern margins of the Ionian abyssal 

plain. 

Despite non-cylindricity and time discrepancies in the tectonic/geodynamic agenda, regional 

cross-sections presented here show also many similarities in the deformation of the lower 

plate between the Tellian edifice in Algeria in the west, the Sicilian Channel between Tunisia 

155

and Italy in the centre, and the Ionian abyssal plain and Eastern Mediterranean Ridge in the 

east. For instance, Late Cretaceous to Paleogene pre-collisional inversions are well 

documented in the autochthonous foreland in the Saharan Atlas, in the Sicilian Channel and 

the Ragusa Plateau, where they predate the development of the overlying Miocene flexural 

basin. Intra-Tortonian inversions are also documented from Sfax in Tunisia to the Sicani 

Mountains in Sicily, as well as in the deep offshore Ionian Basin. Post-suture transpression 

accounts also for late inversions of the underthrust foreland in the Southern Apennines 

(Tempa Rossa and Monte Alpi subthrust prospects), northern Sicily (Panormide-Imerese 

nappes anticline), as well as beneath the Tellian allochthon in Algeria (Bibans and 

Constantinois tectonic windows), whereas transtension and strain-partitioning near the backstop 

have locally led to the development of thrust-top pull-apart basins in the Chelif area 

(Algerian Tell), San'Archangelo Basin (Southern Apennines), as well as on top of the 

Mediterranean Ridge off the western coast of Peloponnesus. 

Whereas slab pull or slab retreat are known to account for foreland flexure and subsidence, 

with deposition and preservation of deep water series in Neogene foredeeps of the 

Maghrebides, Sicily and Apennines, as well as for the present deep water environment of the 

Eastern Mediterranean, slab detachment and further dynamic topography linked to 

asthenospheric rise beneath the Algerian and Tyrrhenian basins have already led to rapid 

uplift and exhumation of the former Tellian, Sicilian and Apenninic foredeeps. 

Ultimately, recent seismic imagery and focal mechanisms help also to document the recent 

development of north-verging thrust faults at the toe of the continental slope from North 

Algerian to North Sicilian margins, thus accounting for a double verging orogen, both the 

Algerian Basin and Tyrrhenian Sea now behaving as retro-arc foreland basins with respect to 

currently active African margin. 

Because recent oil and gas discoveries have been made in the Southern Apennines and Sicily, 

the knowledge of these various structural styles, source rock distribution and timing of their 

maturation should be used as useful analogues when ranking the petroleum potential of early 

foreland closures versus late subthrust prospects in the yet under-explored areas of the 

Algerian foothills (Tell) in the west, and to limit also the exploration risk in the deep Ionian 

offshore and Eastern Mediterranean Basin in the east. 

156




Sedimentology of resedimented carbonates: facies and geometrical characterisation of 

Upper Cretaceous calciturbidite system in Albania 

Rubert Yolaine 1, Jati Mohamed 1, Loisy Corinne 1, Cerepi Adrian 1, Foto Gjergji 2, 

Mushka Kristaq 2 

1, EGID-Bordeaux 3 Institute, 1 allée F. Daguin, 33607 PESSAC Cedex, France 

rubertyolaine@yahoo.fr 

2, Faculty of geology and mining, Tirana Polytechnic University, Albania 

Introduction-Geological setting 

The siliciclastic turbiditic systems have been largely studied motivated by their reservoir 

rock potentials. On the contrary, resedimented carbonates did not benefited of such attention 

but several key studies of resedimented carbonates have permit to precise the facies, the 

depositional models, or the controlling factors (Mullins and Cooks 1986; Einsele et al., 1991; 

Payros and Pujalte, 2008). Nevertheless there are few examples of gravitary limestone works 

notably concerning the geometry due to the lack of continuous outcrops. However 

resedimented carbonates are potential reservoir rocks especially in coarse levels (Mullins & 

Cook 1986; Casabianca et al. 2002). In the south of Albania, Upper Cretaceous limestones 

outcrop and were described as breccia (Llahana Th.; Gucaj A.). The outcropping conditions of 

Piluri, Muzina and Vanister sections studied here, favour a detailed sedimentary study of this 

formation with the facies determination and the geometry description. 

In the SW part of Albania, the Krasta, the Kruja and the Ionian tectonic nappes were 

stacked by a westward NW-SE trending thrusts during the tertiary Alpine orogen (figure 1). 

The western autochtonous Sazani zone corresponds to the pre-apulian platform. Northward 

the tectonic nappes are buried under the post-eocene sediments of the peri-Adriatic depression 

and some formations constitute reservoir rocks for current oil exploitation (Xhavo 2002). 

Piluri, Muzina and Vanister sections are Upper Cretaceous in age and are located in different 

tectonic units (Moisiu & Gurabardhi 2004). Paleogeographically they correspond to slope and 

basin deposits belonging to the Ionian Basin. This basin is bordered in the west part by the 

Apulian platform, and in the east part by the Kruja platform and the transition with basinal 

limestones is faulted (Zappatera 1994). 

Methodology 

In Piluri outcrop, two sections were logged with around 350 m distances (Piluri WSW and 

Piluri ENE) and total thickness reaching 227 m (figure 1). At Muzina two sections were 

logged with 1 km of distance (Muzina-W and Muzina E), the total thickness being about 260 

m. At Vanister around 150 m thick was logged in the upper part of the succession situated at 8 

km NW of Muzina into the same Mali i Gjere massif. For biostratigraphy limit between 

Upper Cretaceous and Paleocene we used the fauna determination of Brahimi et al. (1987) 

and Brahimi et al. (1992). We also use planktonic foraminifera assuming they correspond to 

lesser reworked constituents. 

Results 

Excepted in Piluri-ENE section the four others display three thick levels more or less 

slumped intercalated with decimetric to plurimetric bedded units. These stratified units are t1 

to t4 for the topmost and deformed levels are noted S1 to S3 at the top. For Piluri-ENE section 

a fourth deformed level was identified in the t1 unit (figure 1 & 2). The field sedimentary 

study has allowed to define six facies. 

157

Figure 1 - Geological context (from Moisiu & Gurabardhi, 2004) and panoramas of Upper 

Cretaceous outcrops of Muzina, Vanister and Piluri. 

The Background sedimentation can be described as a clay mudstone with or whithout 

bioturbation but it is difficult to distinguish it from resedimented calcilutite (Einsele et al., 

1991) and we have considered the beginning of bioturbation as the transition between 

resedimented calcilutite and the background sedimentation. 

Fine-, medium- and coarse-grained sequences with thicknesses from 20 to 240 cm were 

observed with a predominant non-erosive base. The fine-grained resedimented carbonates 

include only calcilutitic strata with 20 to 150 centimeter thicknesses, displaying succession of 

undulated lamination and/or planar lamination overlain by a topmost uniform mudstone with 

bioturbations and cherts. The Medium-grained resedimented facies are between 30-200 cmthick 

with normal grading (calcarenite to calcilutite). The sedimentary structures are mainly 

planar and undulated lamination, followed by current ripples. The topmost calcilutitic level 

can show bioturbations and cherts. Coarse-grained sequences are 120 to 240 cm-thick with 

calcirudite to calcilutite granulometry. The base is calciruditic, with mm to cm-scale 

polygenic grains within a calcarenitic matrix, and with normal grading and rarely inverse. 

Topmost intervals are calcarenite to calcilutite with undulated planar and oblique bedding. 

Few cherts are present at the top. 

Cobbly calcirudites without sedimentary structure and internal stratification were observed 

with thicknesses higher than 3 m. The texture appears mud-supported with pluri-millimetric to 

pluri-centimetric polygenic grains included in a calciruditic matrix. Topmost intervals are 

calcarenitic and display sedimentary structures (planar oblique and undulated lamination). 

Through the sections they correspond to the S2 level in Muzina-E section with an erosive base 

displaying slide plane or to the top of deformed levels (above S1 and S3 units) displaying an 

irregular base and a flat top (figure 2). 

Deformed levels were observed in Muzina and Vanister outcrops, with slumped strata 

where sedimentary structures were detected with more or less complete succession as 

described above in stratified beds. In Muzina and Vanister sections, these levels appear 

clearly deformed with folds and slide planes. In Piluri section the outcrop conditions prevent a 

clear distinction of the deformed levels and the deformation is weaker giving an undulated 

aspect and gently folded beds (figure 2). 

158

Figure 2 - Detailed localisation and lithologic sections of Piluri, Muzina and Vanister 

The vertical evolution of sediments in Muzina and Piluri begin with fine-grained beds at 

the base of the unit t1 (figure 2). Then the sediments of the unit 1 become coarser until the 

first slumped level S1. In Piluri-ENE a locally deformed level was detected in unit t1. Above, 

the stratified t2, t3 and t4 units are composed by beds with similar facies than at the top of the 

unit t1. 

Discussion-Conclusion 

The fine- to coarse-grained sequences described above display characteristics relative to 

turbiditic sequences: 1) moderate bioturbation localised in thinner intervals contrary to 

complete bioturbation in contourites (Stow et al. 1998); 2) the scarcity of bottom marks 

typical to calciturbidites; 3) the presence of metric levels of rudites, inverse grading which 

exclude storm deposits; 4) the presence of cherts as nodule or continuous beds (Einsele et al., 

1991); 5) the sedimentary structures succession as in Bouma’s intervals (1962) resulting of a 

decelarating currents. The cobbly levels above S1 and S3 levels seem to show the progressive 

transformation of the mass slide into mass flow. Comparing the three outcrops, lateral 

variations appear implying a proximal character for Piluri: i) the turbidites are thicker and 

159

display rapid lateral variations in thickness and granulometry ii) the average grain size is 

higher; iii) the deformed levels in Piluri are represented by tiled and weaker folded strata. 

The main factors triggering gravitary calcareous systems are tectonism, eustatism or 

sediment supply (Einsele et al., 1991). Regional studies have displayed an important phase of 

instability and resedimentation during the late Cretaceous and later, both in the Ionian Basin 

(Bosellini et al. 1993; Bice et al., 2007) and in the surrounding platforms (Spalluto et al., 

2007; Heba & Prichonnet 2009). The tectonism is evoked as a triggering factor combined 

with a seal-level fall. These instability features can be related to the first movements of the 

compression between African and Eurasian plates beginning in Late Cretaceous (Dercourt, 

1986). 

The comparison of resedimented carbonate in Muzina and Vanister, 8 km apart shows 

relatively few lateral variations in global thicknesses and at the outcrop scale any erosive 

surface marking channel occurrence was observed. Between Piluri and Vanister-Muzina one 

could correlate the third deformed levels (figure 2) but any data allow us to confirm their 

continuity, all the more so in Piluri-ENE a fourth slumped level was observed. Besides the 

total wide of the Ionian basin is around 50 km in the zone (Zappatera, 1994), involving that 

Vanister-Muzina sections could have been fed by the western Sazani and/or the eastern Kruja 

platform. In every instance the quasi-absence of erosive or chanellised features in 

calciturbidites whatsoever their granulometry, contrasts with previous studies about ancient 

submarine fans (Payros and Pujalte, 2008). Besides, lateral variations of facies are weak even 

in Piluri proximal section. Outcrop observations and lateral expansion of the brecciated levels 

detected until the northern part of Mali I Gjere massif (Llahana Th.) might be coherent with a 

spread line-sourced gravitary system (Mullins & Cooks, 1986). 

References 

Bice D.M. et al., 2007, Terra Nova, 19, p. 387-392. 

Bosellini A. et al., 1993, Terra Nova, 5, p.282-297. 

Bouma A.H., 1962. Elsevier, Amsterdam, 168 p. 

Brahimi Q. et al., 1987, Gas and petroleum geological institute of Fier. 

Brahimi Q. et al., 1992, Gas and petroleum geological institute of Fier. 

Casabianca D. et al., 2002, Journal of Petroleum Geology, 25(2), p. 179-202. 

Gucaj A., , Ministry of Mineral ressources and energetics, Institute of Geological 

Research, Gas and Petroleum institute of Fier, Faculty of geology and mining-Polytechnic 

Univeristy of Tirana 

Dercourt J. et al., 1986, Tectonophysics, 123, 1-4, p. 241-315. 

Einsele G. et al., 1991, Springer-Verlag Berlin Heidelberg, New York, 955p. 

Heba G., Prichonnet G., 2009, Bulletin de la Société Géologique de France, 180, n°5, p. 

431-448 

Llahana Th., , Ministry of Mineral ressources and energetics, Institute of Geological 

Research, Gas and Petroleum institute of Fier, Faculty of geology and mining-Polytechnic 

Univeristy of Tirana. 

Moisiu L., Gurabardhi L., 2004, Gas and petroleum geological institute of Fier. 

Mullins H.T. & Cook H.E., 1986, Sedimentary Geology 48 : 37-39. 

Payros A., Pujalte V., 2008, Earth-Science Reviews, 86, p.203-246. 

Spalluto L. et. al., 2007, Sedimentary Geology 196, p.81-98. 

Stow D.A.V. et al., 1998, Sedimentary Geology, 115, p.3-31. 

Xhavo A., 2002, National Petroleum Agency, Tirana, 24p. 

Zappaterra E., 1994, AAPG Bulletin, 78, n°3, p. 333-354. 

160




Reservoir properties of resedimented carbonates of Upper Cretaceous turbiditic 

system in Albania 

Rubert Yolaine 1, Jati Mohamed 1, Loisy Corinne 1, Cerepi Adrian 1, Foto Gjergji 2, 

Mushka Kristaq 2 

1, EGID-Bordeaux 3 Institute, 1 allée F. Daguin, 33607 PESSAC Cedex, France 

rubertyolaine@yahoo.fr 

2, Faculty of geology and mining, Tirana Polytechnic University, Albania 

Introduction-Geological setting 

The siliciclastic turbiditic systems have been largely studied motivated by their reservoir 

rock potentials contrary to resedimented carbonates which did not benefit of such attention. 

But several key studies of modern and ancient resedimented carbonate systems have permit to 

precise the facies, the depositional models, or the controlling factors (Mullins and Cooks 

1986; Einsele G. et al., 1991; Payros and Pujalte, 2008). Studies about resedimented 

carbonates have allow to demonstrate their reservoir rock potential especially in coarse levels 

(Casabianca et al. 2002). 

The Northeastern part of Albania is an hydrocarbon bearing province with in particular 

Late Cretaceous limestones which host oil reservoirs under the Peri-adriatic depression 

(Xhavo, 2002). More in the south, this formation outcrops and is described as brecciated 

limestones. In the Kremenara anticline, this formation displays superficial oil seeps (Dewever 

et al. 2007) which allowed to describe the porosity and the factors controlling its formation. 

The outcrops of Piluri and Muzina, studied here are devoid of oil seep but outcropping 

conditions favour a combined sedimentary and petrographical-petrophysical study of the 

Upper Cretaceous brecciated carbonates. A preliminary sedimentological study of these 

brecciated limestones allowed to determine their gravitary origin. Paleogeographically they 

correspond to slope and basin deposits belonging to the Ionian Basin (Zappatera, 1994). 

Methodology 

In Piluri outcrop, two sections were logged with total thickness reaching 227 m. At Muzina 

two sections were logged, the total thickness being about 260 m. At Vanister around 150 m 

thick was logged in the upper part of the succession. Several facies were defined by 

sedimentological. study: fine-, medium- and coarse- calciturbidites, debris-flows, and slumps. 

Sampling was performed relatively to each field facies and uncovered, unpolished thin 

sections were made and observed with an optical microscope (Olympus BH-2). Petrophysical 

measurements were realised with an air permeameter IPF 49 apparatus and dried cores, and 

with a mercury porosimeter Micromeritics III and dried rocks fragments. 

Results 

Petrography 

Thin section examination allowed to define seven microfacies, the various constituants and 

to describe the diagenesis with additionaly field observations. 

161

Figure 1 – Geological context of the Upper Cretaceous calciturbidites (Moisiu & 

Gurabardhi, 2004) 

Microfacies 1-Radiolarian mudstone: they correspond to radiolarian mudstone with some 

pelagic foraminifera, oxides and collophane fragments. 

Microfacies 2-Mudstone to fine wackestone: the grains are around 50 µm with stratiform 

grain orientation, in a micritic matrix. The identifiable fauna is pelagic foraminifera. It was 

encountered in fine-grained turbidites and in finer intervals of medium- and coarse-grained 

intervals (i.e. Te interval). 

Microfacies 3-Laminated wackestone: it displays an oblique or stratiform lamination with 

a 100-200 µm granulometry range. The fauna is both of shallow water and deeper water with 

pelagic foraminifera. It is associated to medium-grained and coarse-grained turbidites (i.e. Tb 

to Td intervals). 

Microfacies 4-Grain oriented bioclastic/lithoclastic wackestone-floatstone: the sorting is 

poor, the granulometry is around 300µm to 2mm and a grain orientation occurs. The 

identified fauna is both of shallow water and deep water. Platform extraclasts and some 

mudclasts were also observed. This microfacies is associated to Tb to Td intervals of mediumgrained 

and coarse-grained turbidites. 

Microfacies 5-Bioclastic/lithoclastic wackestone-floatstone: the grains (mean >1mm) are 

poorly sorted and consist of shallow and deep water bioclasts, turbiditic microfacies-like 

intraclasts and plate-forms extraclasts. This microfacies was encountered in mud-flow levels, 

in coarser intervals such as Ta of Bouma (1962) or in topmost of very coarse-grained 

calciturbidites. 

Microfacies 6-Bioclastic/lithoclastic packstone-rudstone: the sorting is moderate to poor, 

the mean granulometry is higher than 300 µm. The components are bioclasts of shallow and 

deep water settings and in a lesser degree lithoclasts with mainly extraclasts. This facies is 

associated with the coarser intervals (i.e. Ta-Tb) of medium- and coarse-grained turbidites. 

Microfacies 7-Extraclastic floatstone-rudstone: the sorting is poor, the granulometry is 

millimetric to centimetric. The lithoclasts represented by shallow-water extraclasts are 

numerous relatively to bioclasts. The bioclasts are of deep-water and shallow water origin. 

This microfacies was observed locally in three coarser levels (Ta or Tb) of coarse-grained 

turbidites. 

The consituants of calciturbidites are more or less fragmented fauna and lithoclasts. 

Shallow-water tests commonly encountered are rudists, large-shelled bivalves and benthic 

foraminifera (miliolids, rotaliids, orbitoides and siderolites sp.) with some omphalocyclus 

162

macroporous sp., lepidorbitoides sp., sulcoperculina sp. (Heba G., personal comm.). The deep 

water fauna is essentially represented by planctonic foraminifera. Lithoclasts are represented 

by extraclasts with various facies: mudstone with fenestrae vugs, mudstone with ostracode 

fragments, mudstone with miliolids sp., packstone-grainstone with micritised benthic 

foraminifera (miliolids, textularids), grainstones containing shallow water fauna. Locally 

some lithoclasts are interpreted to calciturbidites like intraclasts (laminated wackestonespackstones 

with foraminifera, pelloids, and thin-shelled debris). 

The post-resedimentation diagenesis is weak because of the mud-rich facies. Pressure 

solution features were observed in rudstone textures with grain contacts. In mudstone to 

packstone textures stratiform stylolites are common. In Tb to Td intervals of calciturbidites a 

phase of recristallisation occured with local microsparite then sparitic calcite. The field 

observations allow to display that sparite recristallisation and cherts formation occur very 

early in the diagenetic evolution because they appear dislocated and distorted in slumped 

levels. A later fracturing phase was observed at outcrop scale in Muzina section, with reverse 

faults oriented globally N150E with apparent dip around 60E. At the bed scale a fracture 

generation displays azimuth around N050E and dips from 70° toward NW to vertical. Another 

fracture generation relatively less mineralised with azimuth N130E and sub-vertical dips was 

detected but any obvious chronology was observed between the both generations. Vertical 

stylolites are present with directions around N135E. The orientation of veins and stylolites are 

coherent with a compressive regime in the N040E-N050E direction and these microstructures 

are consistent with the outcrop-scale reverse faults. 

Reservoir properties 

In thin section the porosity is visually weak (

Figure 2 – Example of porosity measurements realised on a calciturbiditic sequence and 

thin section photographies 

The diagenesis of the resedimented carbonates is slight visible owing to the mud-rich 

facies which prevents the precipitation of diagenetic cements. This diagenesis is mainly 

marked by compactionnal stylolites and recristallisation calcite in laminated intervals of 

calciturbidites. Which is interesting is the early setting up of the chert and the calcite 

recristallisation before the slumping phase. This significates here that these diagenetic 

processes occur in the first decameters of sediment depth. 

The petrophysical measurements demonstrate a relatively weak matrix porosity which is 

due in great part to the mud-rich facies. Besides, the pores are globally disconnected with 

important trapped porosity. This demonstrates that matrix porosity does not act as fluid 

pathways. In the contrary, at the outcrop-scale numerous fractures and stylolites could act as 

fluid pathways through the calciturbiditic strata as previously described in the northern zone 

(Grahams Wall et al. 2006). The fracturation phase shows directions and movements coherent 

with the alpine tertiary orogen (Kilias et al., 2001). 

References 

Bouma A.H., 1962. Elsevier, Amsterdam, 168 p. 

Carannante G. et al., 2000, Sedimentary Geology, 132, p.89–123. 

Casabianca D. et al., 2002, Journal of Petroleum Geology, 25(2), p. 179-202. 

Dewever B. et al., 2007, Sedimentology, 54, p.243–264. 

Einsele G. et al., 1991, Springer-Verlag Berlin Heidelberg, New York, 955p. 

Kilias A. et al., 2001, Journal of Geodynamics, 31, p.169-187. 

Moisiu L., Gurabardhi L., 2004, Gas and petroleum geological institute of Fier. 

Mullins H.T. & Cook H.E., 1986, Sedimentary Geology 48 : 37-39. 

Payros A., Pujalte V., 2008, Earth-Science Reviews, 86, p.203-246. 

Ruberti D., 1997, Sedimentary Geology, 113, p.81-110. 

Schlüter M. et al., 2008, Cretaceous Research, 29, p.100-114. 

Stow D.A.V. et al., 1998, Sedimentary Geology, 115, p.3-31. 

Xhavo A., 2002, National Petroleum Agency, Tirana, 24p. 

Zappaterra E., 1994, AAPG Bulletin, 78, n°3, p. 333-354. 

164




SHALLOW and DEEP CONTROL on the THERMAL STRUCTURE of BASINS as 

INFERRED by 3 D NUMERICAL MODELS: EXAMPLES from the CENTRAL 

EUROPEAN BASIN SYSTEM 

Magdalena SCHECK-WENDEROTH (1) , Mauro CACACE (1,2) , Yuriy MAYSTRENKO (1) 

and Björn LEWERENZ (1) 

(1) Helmholtz Centre Potsdam – GFZ German Research Centre for Geosciences, 

Telegrafenberg, D-14473 Potsdam, Germany, (leni@gfz-potsdam.de), 

(2) University of Potsdam, Am Neuen Palais 10, D-14473 Potsdam, Germany 

The long term availability and the large extent of geothermal heat make it an attractive source 

for a sustainable supply of energy. However, exploitation of geothermal energy requires a 

quantitative resource assessment that must provide a correct identification of the main 

physical transport mechanisms involved. To understand the thermal regime on a basin-scale, 

we perform 3D numerical simulations of heat transport processes for different areas of the 

Central European Basin System. Our results provide new insights on the major controlling 

factors of the thermal field and indicate that lithosphere-scale factors are superposed with 

effects resulting from the spatial interaction of thermal rock properties and corresponding 

layers’ geometry in the basin. A detailed model describing the geometry of the main 

stratigraphic layers is used to properly constrain the lithology-dependent thermal rock 

properties. Based on this geological model, the 3D present-day regional conductive 

geothermal structure of the basin is simulated. We assess the sensitivity with respect to 

contrasting thermal rock properties in the sediment fill and with respect to the influence of 

different configurations of the crust and lithospheric mantle. We find that small wavelength 

variations (up to a few kilometers) in the shallow thermal and heat flow fields are mainly 

influenced by the respective thickness and geometry of a salt layer present in the succession. 

The chimney effect of the highly conductive salt is counteracted by the isolating effects of 

salt-rim syncline sediments. In contrast, the long wavelength character (> 50 km) of the near 

surface heat flow and temperature distribution is controlled by the configuration of the crust 

and upper mantle beneath the basin. 

165

166




The DINARIDES-HELLENIDES as a PART of the CARPATHIANS-ALPS SYSTEM: 

ANCIENT and RECENT REORGANIZATIONS of a COMPLEX SYSTEM of 

MOUNTAIN CHAINS 

SCHMID Stephan M. 1 , BERNOULLI Daniel 2 , FUGENSCHUH, B. 3 , MATENCO L. 4 , 

OBERHANSLI, R. 5 , SCHEFER, S. 2 and USTASZEWSKI K. 6 

1 

Geologisch-Paläontologisches Institut Universität Basel & Geophysical Institute ETH 

Zürich, Switzerland, Stefan.Schmid@unibas.ch 

2 

Geologisch-Paläontologisches Institut Universität Basel, Switzerland, 

Daniel.Bernoulli@unibas.ch & Senecio.Schefer@unibas.ch 

3 

Geology & Paleontology Innsbruck University, Austria, Bernhard.Fuegenschuh@uibk.ac.at 

4 

Department of Tectonics Vrije Universiteit Amsterdam, The Netherlands, 

liviu.Matenco@falw.vu.nl 

5 

Institut für Geowissenschaften Universität Potsdam, Germany, roob@geo.uni-potsdam.de 

6 

GFZ German Research Centre for Geosciences, Potsdam, Germany, kamilu@gfz- 

potsdam.de 

A previously published tectonic overview of the Alps, Carpathians and Dinarides (Fig. 1; 

Schmid et al. 2008) is extended to the Hellenides and further into the Taurides and Pontides of 

Western Turkey. We focus on the discussion of along strike similarities and differences of this 

orogenic system. Some of the differences are due to ancient (i.e. pre-Miocene) reorganizations 

related to the opening and closing of the various branches of Tethys (Alpine Tethys, 

Neotethys, Paleotethys). Others, however, are due to young and rather dramatic modifications 

of a pre-existing orogenic system. Such Miocene to recent reorganizations are associated with 

processes of slab break-off and/or slab-roll back, backarc extension and substantial strike-slip 

displacements between large composite blocks or microplates such as the so-called Alcapa, 

Tisza and Dacia Mega-Units. 

The Dinarides are juxtaposed with the Alps along the present-day Mid-Hungarian fault zone 

(a former transform fault). The Dinarides represent an orogen of opposite subduction polarity 

with respect to the Alps. Since about 20Ma ago the easternmost Alps acquired the Dinaridic 

subduction polarity, whereby Adria now represents the lower plate (Ustaszewski et al. 2008). 

The architecture of the Dinarides can be traced into the Hellenides without difficulty. Major 

along strike lateral changes are modest and the main problems encountered during 

compilation are of nomenclatural nature since the names given to the various units 

unfortunately change every time a national boundary is crossed. Both Dinarides and 

Hellenides consist of thrust sheets that formed in Late Cretaceous to Cenozoic times and are 

built up of Adria-derived continental material and previously obducted ophiolites. These 

thrust sheets are located in a lower plate position with respect to the upper plate, i.e. the Tisza 

and Dacia Mega-Units in the northern and southern Dinarides, respectively, and, at least 

temporarily, by the Rhodopes including the Circum-Rhodope belt in the Hellenides (e.g. van 

Hinsbergen et al. 2005). The latter extend eastwards into the Pontides of Western Turkey 

(Okay 2008). All these upper plate Mega-Units have European affinities. However, those in 

the east also incorporate older sutures formed during the closing of Paleotethys. These upper 

plate units are separated from the lower plate units, i.e. the units that are commonly referred to 

167

as the Dinarides or Hellenides by a Late Cretaceous to Early Paleogene suture zone (named 

Sava Zone), which represents that part of the northern branch of Neotethys (the Meliata– 

Maliac–Vardar Ocean; Schmid et al. 2008) that stayed open until end-Cretaceous times. 

The along-strike changes noted when going from the Dinarides into the Hellenides are 

relatively minor and gradual: (1) The pelagic Pindos through, which most probably represents 

a pelagic seaway underlain by thinned continental crust is absent in the Dinarides north of 

Dubrovnik and starts to broaden southwards, located between shallow-water carbonate buildups 

(the Pelagonian and the Gavrovo-Tripolitza realms); (2) The amount of Miocene 

shortening affecting southwestern-most foreland, associated with the Aegean roll-back, 

dramatically increases southwards across the Skutari-Pec and the Cephalonia transfer zones; 

(3) The Hellenides contrast with the Dinarides by the presence of two intracontinental highpressure 

belts that are absent in the Dinarides: an inner one of Eocene age (Cycladic 

Blueschist Belt) that can be traced into Turkey and an outer one of Miocene age only found 

between the Peloponnesus and Crete. 

The Sava zone of the Dinarides can be followed along strike all the way into the Izmir-Ankara 

suture zone. In the Dinarides and Hellenides parts of the ophiolites of the northern branch of 

the Neotethys Ocean were obducted already during the latest Jurassic onto the Adriatic 

margin (Western Vardar Ophiolitic Unit) and were subsequently involved in Late Cretaceous 

to early Paleogene thrusting. This led to the formation of composite nappes that consist of 

continent-derived material in their lower part and ophiolites in their upper part. During the 

latest Jurassic other parts of the Vardar Ocean (Eastern Vardar Ophiolitic Unit) were also 

obducted and thrust onto the European margin (i.e. the Dacia Mega-Unit). Our one-ocean 

concept does not require the presence of “terranes” separating various oceanic branches along 

the Neotethys margin, such as the Drina–Ivanjica block or the Pelagonian “massif”. These 

continental units simply represent tectonic windows of the distal Adriatic margin located 

below the obducted ophiolitic thrust sheets. Moreover, there is no need for a separate ocean 

linked with the Meliata–Maliac ophiolites, because these remnants simply represent the 

Triassic-age parts of the Vardar Ocean, preserved as slices within or below ophiolitic 

mélanges accreted in front of the obducted Western Vardar ophiolites. This one-ocean logic 

can be followed all the way from the Western Carpathians and Dinarides into the Hellenides. 

In the Hellenides and in Western Turkey we find no evidence for a Pindos oceanic lithosphere 

(i.e. for the so-called “Pindos Ocean”). The derivation of the protoliths of the Cycladic 

Blueschists (predominantly marbles and Triassic? mafics), generally also attributed to the 

Pindos “Ocean”, from oceanic crust is highly questionable. 

A very major change occurs, however, between the Hellenides and the Anatolides–Taurides 

of Western Turkey. In Turkey, as well as in the Greek islands of Karpathos and Rhodes, 

ophiolite obduction clearly occurred during the Late Cretaceous rather than in the Late 

Jurassic (Koepke et al. 2002; Okay 2008) and was associated with blueschist facies 

metamorphism in the immediately underlying accretionary wedge in Western Turkey 

(Tavsanli blueschist belt). This suggests the presence of an old and not yet understood major 

along strike change located somewhere in the easternmost Aegean. On the other hand the 

Cycladic Blueschist Unit that paleogeographically represents formerly subducted parts of the 

Pindos pelagic seaway can easily be traced from the island of Samos into Western Turkey 

(e.g. Rimmelé et al. 2004). There the Cycladic Blueschist Unit overlies the Menderes 

“Massif”, probably representing the eastern continuation of the Gavrovo–Tripolitza Zone. The 

so-called Lycian nappes that tectonically overlie both the Menderes “Massif “ and the 

Cycladic Blueschist Unit contain an older, i.e. latest Cretaceous-age blueschist unit (Ören 

Unit) at their base. It is suggested that this Ören blueschist belt can be laterally followed into 

the Afyon Zone further to the northeast that borders the northern edge of the nonmetamorphic 

Taurides (Pourteau et al. 2010a,b). The higher and non-metamorphic parts of the 

168

Lycian nappes possibly represent an eastern equivalent of the Pelagonian Zone. They are also 

overlain by ophiolites that were obducted before final nappe transport in the Cenozoic. 

However, obduction occurred in Late Cretaceous (and not Late Jurassic) times in the case of 

the Lycian nappes. According to this hypothesis, both the Pelagonian Zone and the northern 

passive margin of the Anatolide–Tauride Block (Lycian nappes) would be part of one and the 

same micro-plate (or two laterally adjacent microplates), referred to as Adria microplate in the 

Western Mediterranean and Anatolide–Tauride Block in the Eastern Mediterranean. Both 

would represent pieces of Gondwana that broke off the African plate along the opening of the 

southern branch of Neotethys (Okay 2008, Handy et al. 2010). 

Another major along-strike change concerns the southeastern continuation of the Carpatho– 

Balkan orogen, a Lower Cretaceous orogen that is located in an upper plate position in respect 

to the Dinarides-Hellenides. This east-verging older orogen tectonically overlies the 

Rhodopes and it is not yet clear if it can be traced further to the southeast and into the socalled 

Circum-Rhodope Belt. The Rhodopes also represent a part of the European margin and 

hence originally also were northerly adjacent to the Meliata–Maliac–Vardar branch of 

Neotethys. However, in contrast to the thrust sheets making up the Dacia Mega-Unit that 

overlie the Moesian plate, the Rhodopes were subducted northward below Moesia and 

subsequently exhumed as a huge core complex surrounded by normal faults. Hence, the 

Rhodopes formerly were a lower plate unit that was subducted very early on (possibly as early 

as during the Jurassic) and that is only present in the Hellenides but not in the Dinarides. 

Possibly the Rhodopes, or alternatively only the lower part of them (Drama block), formerly 

bordered an ocean that was located north of the Meliata–Maliac–Vardar branch of Neotethys. 

This more northerly located ocean that only appears when going eastwards into the hinterland 

of the Hellenides and Anatolides–Taurides either was a branch of Neotethys that was 

originally located to the north of the Meliata–Maliac–Vardar branch of Neotethys, or 

alternatively, was a part of the Paleotethys. 

References 

Handy, M.R., Schmid, S.M., Bousquet, R., Kissling E. & Bernoulli, D. (2010). Reconciling 

plate-tectonic reconstructions of Alpine Tethys with the geological-geophysical record 

of spreading and subduction in the Alps. Earth Science Reviews in press. 

Koepke, J., Seidel, E. & Kreuzer H. (2002). Ophiolites on the Southern Aegean islands Crete, 

Karpathos and Rhodes: composition, geochronology and position within the ophiolite 

belts of the Eastern Mediterranean. Lithos 65: 183– 203. 

Pourteau, A., Candan, O., Oberhänsli, R. & Sudo, M. (2010a) 40Ar/39Ar dating of 

subduction-related metamorphism in the Anatolide HP belt, W-Turkey: implications for 

the evolution of the Eastern Mediterranean. EGU Vienna Abstract EGU2010-3996. 

Pourteau, A., Candan, O. & Oberhänsli, R. (2010b). Paleotectonic reconstruction of the 

Neotethyan suture in Western-Central Turkey. Tectonics : doi:10.1029/2009TC002650, 

in press. 

Okay, A.I. (2008). Geology of Turkey: A synopsis. Der Anschnitt 21: 19-42. 

Schmid, S.M., Bernoulli, D., Fügenschuh, B., Matenco, L., Schefer, S., Schuster, R., Tischler, 

M. & Ustaszewski, K. (2008). The Alpine-Carpathian-Dinaridic orogenic system: 

correlation and evolution of tectonic units. Swiss Journal of Geosciences 101:139-183. 

Rimmelé, G., Parra, T., Goffé, B., Oberhänsli, R., Jolivet, L. & Candan O. (2004). 

Exhumation paths of high-pressure–low-temperature metamorphic rocks from the 

Lycian Nappes and the Menderes Massif (SW Turkey): a multi-equilibrium approach. 

Journal of Petrology 46: 641-669. 

169

Ustaszewski, K., Schmid, S.M., Fügenschuh, B., Tischler, M., Kissling, E. & Spakman, W. 

2008: A map-view restoration of the Alpine-Carpathian-Dinaridic system for the Early 

Miocene. In: Orogenic processes in the Alpine collision zone (N. Froitzheim & S.M. 

Schmid, editors), Swiss Journal of Geosciences 101/Supplement 1: S273–S294. 

van Hinsbergen, D.J.J., Hafkenscheid, E., Spakman, W., Meulenkamp, J.E. & Wortel, R. 

(2005). Nappe stacking resulting from continental lithosphere below subduction of 

oceanic and Greece. Geology 33:325–328. 

170

Figure 1: Major tectonic units of the Alps, Carpathians and Dinarides (from Schmid et al. 

2008). 

171

172




CORRELATION of the WESTERN STRUCTURES of IONIAN ZONE and the 

RELATION with AFRICAN PLATE (ADRIA MICRO PLATE) 

Afat SERJANI & Agim GUCAJ, 

Geological Survey of Albania, Tirana, Albania 

E-mail: aserjani@yahoo.com 

INTRODUCTION 

The workshop on sedimentary basins, dynamics and active geological processes is for the 

authors of this presentation a good chance to review the image of the southwestern 

geological structures of Ionian Zone (known as Çika anticline belt). Authors have worked 

for long time in ex-Gjirokastra Geological Enterprise leading geological prospecting for 

sedimentary solid mineral ores. 

Geological structures of Çika anticline belt are correlated forming structural chains in 

continuation of common northwest-southeast to Greece. Longitudinal faults, especially 

those of typically thrust character testify that Mesozoic carbonate formations of Ionian 

Zone, are swimming on the evaporate substratum, which lies directly on the basement of 

the oldest, Permian formation. This basement below evaporate rocks, may have important 

interest in hydrocarbon generation and trapping, amongst the other known upper levels. 

The main function in geodynamic processes of structural chains have played mutual 

interaction between African Plate (Adria micro plate) or Sazan-Karaborun shallow water 

carbonate platform and Orogen (Eurasian Plate). The subduction of the platform to the 

southeast, underneath the Orogen, it is supposed to get down east up to central part of 

Ionian Zone, just there where is Leshnica-Zhulat-Vermiku thrust fault, accompanied by 

salt formation, by volcanic and metamorphic rocks. 

Geodynamic processes of this contact are analogues as the relations between Hellenic 

Trench and Eurasian Plate south, in Greece, according which there are generated 

earthquakes in both countries. 

Underneath Fterra and Çika over thrusts we suppose buried in depth, western flanks of 

these structural chains. 

FORMER PUBLICATIONS and INTERPRETATIONS 

Ionian Zone for long time has been object for prospecting of hydrocarbons and solid 

sedimentary ores, especially during the intensive development of geological works and 

studies in Albania (1960-1990). Last years, the authors have done the correlation of 

geological sheets between Albania and Greece. By Gjirokastra Geological Branch, 

geological maps in scale 1: 50 000 of Gjirokastra, Delvina, and Saranda regions there are 

compiled. The new conception of the anticline and syncline structural chains, located 

opposite each other is put. Structural chains are built by some structural units, placed one 

after the other in form of steps. 

173

In new geological map of Albania (in sc. 1: 200 000), the eastern contact of Ionian Zone 

and the age of evaporate substratum there are presented by mistake. Melesini carbonate 

massif east belongs to Ionian Zone (Misha V., 1975, Serjani A., 1984), and Permian age 

of evaporate substratum is determined (Diamanti F., 2002). 

In “Thrust Tectonics in Albania” Symposium, held in Tirana ( November, 1990), 

Prrenjasi E. (1991) emphasized that limestones are covered under the lower flank of 

structures, Tushaj D. et al. (1991) represented carbonate platform (Adria micro plate) 

plunged deep to the east below Orogen up to the Vlora-Elbasani-Dibra transversal fault, 

retrocharriages from west to the east were presented as well (Serjani A., 1991) . 

Papazachos V. K. (2001) argued the distribution of earthquakes along with the contact of 

Hellenic Trench with Eurasian Plate and further northwest along with the contact of 

Apulian Plate (Adria micro plate) with Orogen (Eurasian Plate) as well. 

K. A. Nikolaou (2001), determined as the most important factors of hydrocarbon 

generation: the reversible and thrust faults and evaporates. V. Karakitsios, et al. (2001), 

as main source of hydrocarbons determined amonitico rosso of Toarian, and a specific 

horizon inside the evaporates. They suppose that “the potential traps are related to small 

anticlines…” D. Mountrakis (2001) has put the idea that during the orogenic processes of 

Alpine–Meogean, a migration towards the southwest direction of compression and 

extension tectonic events caused the successive subduction towards the southwest. 

The CORRELATION of the STRUCTURAL CHAINS 

The authors argue that as all over Ionian Zone, in this area, structures were formed in 

form of anticline and syncline chains, but later, tectonic events deformed their forms and 

primary position. The main structural chains west of Fterra thrust there are as following 

(Fig. 1, 2): 

-Syncline chain: Fterra-Shen Vasil-Aliko-Livadhja-Shales-Sajadha Bay in Greece. Below 

thrust plane to the east of this syncline chain must be buried the western flank of Fterra 

anticline chain, jumping and splitting. 

-Anticline chain: Qeparo-Kakome-Butrint-Çiflig-Pagane in Greece. Bogazi anticline and 

Mile-Bufi structural nose are part of eastern flank of this anticline chain. 

-Syncline chain: Kudhes-Butrinti Bay-Southeastern limit of Korphy Island. 

-Anticline chain: Çika-Pilur-Korphy. On the surface it is outcropped only eastern flank, 

placed directly on the thrust plane. Only in Llogara Pass thrust fault coincides with the 

contact between African Plate (Adria micro plate) and Orogen. Below Çika thrust fault, 

underneath the eastern flank, it is buried western flank of this anticline chain, and Dukati 

syncline chain. 

-Syncline chain: Dukat-Western Korphy, which is compressed and buried because of the 

collision of Adria Platform with Orogen. We think that this chain it is wider and covered 

in depth. 

In above mentioned structural chains there are variation and inclinations of the crest lines 

as result of orogenic polarity, and may be there are formed small structures and structural 

noses, but all times belonging to the same structural chain. 

174

SEISMOGENIC DEEP FAULTS in IONIAN ZONE 

The main seismogenic faults in Ionian zone from east to the west there are: 

1. Seismogenic fault: Konica-Çarshova-Çorovoda-Ishmi Gorge. 

2. Berati thrust fault: Janina-Glina-Dragot-Lushnje–Lales Bay. 

3. Central thrust fault of Mali Gjere-Kurveleshi: Leshnica-Delvina-Zhulati-Gusmari- 

Vermiku-Bashaj-Selenica-Karavasta Bay. 

4. Sajadha-Livadhja-Shen Vasil-Fterra-Matogjini, where it is crossed with central 

Kurveleshi fault north. 

5. Western thrust fault: Korphy Island-Dhermi-Llogara-Vlore-Seman, according which 

Çika anticline chain was thrusted northwest. 

6. At last, to the west it is outcropped the subduction contact of African Plate (Adria 

micro plate) with Orogen (Eurasian Plate), which in continuation to the depth east joined 

up with the others thrust faults. Evaporate rocks are sprained along with thrust faults up 

to the high levels (1300-1500m). Along with planes of thrust faults, in most cases there 

are big water springs. The main transversal seismogenic faults there are: Vlora-Elbasan- 

Diber, Borsh-Kardhiq, and that in center of Korphy Island. 

RELATIONS between PLATES 

By the collision of African Plate (Adria micro plate) with Eurasian Plate during Cenozoic 

period, the plates were break, crushed, especially in places next to the contact of 

subduction, and were formed micro plates and micro blocks, and displacements of thrust 

character, along with deep thrust faults. 

The contact between African Plate and Orogen outcrops only in Llogara, where coincides 

with Çika thrust fault and in Cefalonian islands in Greece. To the north and south it is 

difficult its location, and it is more difficult to determine how long and how much deep to 

the east it is subducted platform underneath the evaporate substratum of Ionian Zone, and 

what relation it has with evaporates and with their basement. 

Commonly, it is supposed, that platform it is plunged below Pre Adriatic Depression 

(PAD) and South Adriatic Basin up to the Vlora-Elbasan-Diber transversal fault (Shtreto 

Th., et al., 1995, Mehillka Ll., et al., 1995, Tushaj D., et al., 1991), or it is supposed up to 

the central fault of Kurveleshi Belt, below the “Miocene basin depocenter” (Guri S., et 

al., 1995). 

During Liass period, as result of opening of Pangea, the extension forces caused the 

formation of the deep faults of southeast-northwest direction and creation of differenced 

bottom of Ionian Basin, with horsts and grabens. In Çika anticline chain the 

differentiation was bigger, and the basin was relatively less deep. That is reflected in the 

small thickness of deposits and in breaks in sedimentation. 

During Tortonian, the compression forces riche their maximum and caused the final 

folding of deposits. We think that the folding of Ionian Zone, may be it is more early, as 

result of subduction of Neotetis oceanic crust below Cimmeriane-Euroasian Plate since 

the Cretaceous-Paleocene and by the collision and subduction of Adria micro plate 

underneath Alpine-Cimmerian-Eurasian Plate during Miocen-Pliocen (Mountrakis D., 

2001). The subduction of Adria caused reversible thrusts, retrocharriages (Serjani, A. 

1991, Velaj, T. et al.,1999). According the paleomagnetic studies (C. Kissel, C. Laj, 

175

1991), Preapulian and Ionian zones have undergone two successive clockwise rotations 

of about 25 o each, of Middle Miocene and Plio-Quaternary ages respectively. This period 

coincides with the subduction of the Adria micro plate underneath Ionian Orogen. 

External zones of Albanides and Hellenides, during last 15 My have been affected by 

displacements which are much more rapid and of much larger amplitude than it is 

supposed by geological and geophysical studies. 

Sazan-Karaborun platform (Adria micro plate) it is plunged deep east below the central 

part of Ionian Zone, compressing strongly carbonate formation, folding and crushing it, 

evaporate substratum and terrigenous basement of Permian age below evaporates. By 

strong compression salt formation was squeezed up to the surface along with thrust faults. 

While in central Kurveleshi fault, by the compression from both sides were squeezed to 

the surface fragments of basement with volcanic and metamorphic blocks and windows 

of pink color terrigenous series of Permian. We consider this series named “motley serie” 

(Seria laramane”) by Isa Bajo (1984) as the basement of evaporate substratum. 

Lithological content and color are similar with Permian deposits all over Mediterranean 

Basin. Stratigraphical and space position of this series coincides with the bottom of salt 

rocks. The “Cap rock” is formed at the top of evaporate substratum, while this pinkish 

packet it is placed at the bottom of gypsum rocks. The absolute geological age, according 

the strontium isotope analysis is Lower Permian (the end of Wordian or Middle 

Changshigian: 252.5-246My) for Peshkopi, and Middle Permian, Lower Artiskian 

(266.5My) up to Lower Triassic (245 My) for Dumrea gypsum (Diamanti F., 2002). The 

hypothesis of Permian age as basement of evaporates is done and argued before (Bajo I. 

1984, Serjani and Bajo, 1994). At last, it is important to note, that the famous Albanian 

specialist of tectonic, and the highest authority in geology of Albania, Prof. Vangjel 

Melo, since the first view of this packet has given the option of Permian age. 

Just this basement below evaporate rocks, due to its lithological content and 

stratigraphical position may have important interest in hydrocarbon generation and 

trapping, amongst the other known upper Mesozoic levels. 

CONCLUSIONS 

In southwestern part of Ionian Zone structures are not separated, but they form regular 

anticline and syncline chains of southeast-northwest direction. Their crest lines change 

level along with strike down and up, in form of steps. 

Deep seismogenic faults, have a thrust character from southeast to northwest, but by the 

subduction of Adria micro plate underneath the Orogen, retrocharriages from westnorthwest 

to east-southeast are happened. 

Çika and Fterra thrust faults have buried western flanks of anticline chains below the 

eastern flanks. Parts of the next syncline chains are buried as well. 

Adria micro plate it is sub ducted deep to the east up to the central part of Kurveleshi 

anticline belt, jumping and squeezing evaporite substratum and terrigenous basement of 

Permian. The basement below the evaporate substratum, constitute may be a new 

interesting level for hydrocarbon generation and trapping in Ionian Zone. 

REFERENCES 

1. Bakiaj H., Bega Z., 1991. Bul. Shk. Gjeol. Nr. 1 Tirane. 

176

2. Bajo I., 1984. Evaporitet e zones Jonike. Thesis. Gjirokaster. 

3. C. Kissel, C. Laj. 1991. Geodynamic and Tectonic Evolution of Northern Greece from 

Korphy to Thraki: A Paleomagnetic Approach. Bul. Shk. Gjeol. Nr. 1. 

4. Diamanti F. 2002. Formacioni evaporitik ne Shqiperi dhe mundesia e kurthezimeve 

hidrokarbure. Bul Shk. Gjeol. Nr. 2, Tirane. 

5. Guri S., et al.1995.A summary on geological setting of the Pre-Adriatic Foredeep. 

Proceedings: Current and Future Problems of oil industry in Albania. Fier. 

6. Karakitsios V., Rigakis N. Bakoupulos I. 2001. Migration and trapping of the Ionian 

series Hydrocarbons (Epirus, NW Greece). The 9-th I. C., Athens. 

7. Mehillka Ll. Seiti H., Veizaj V. 1995. Tectonic evaluation of External Albanides. 

Proceedings: Current and Future Problems of oil industry in Albania. Fier. 

8. Mountarkis D. 2001. Tectonic evolution of the Hellenic Orogen. Geometry and 

Kinematics of the Deformations. The 9-th I. C. Athens. 

9. Nikolaou K. A. 2001. Origin and Migration Mechanism of the main Hydrocarbons seeps 

in Western Greece. The 9-th I. C. Athens. 

10. Papazachos V. K. 2001. Active Tectonics in the Aegean and Surrounding Areas. The 9-th 

International Congress, Athens, September 2001. 

11. Prrenjasi E., Misha V., Bregu H. 1991. Stili tektonik dhe modeli strukturor i rajonit te 

Sarandes. Bul. Shk. Gjeol. Nr. 1, Tirane. 

12. Serjani A., Gucaj A., Husi R., 1986. Te dhena e mendime per tektoniken e brezit 

anticlinal te Kurveleshit. Bul. Shk. Gjeol. Nr. 3. Tirane. 

13. Serjani A., 1991. Aspekte te tektonikes mbihypese nga perendimi ne lindje ne 

rrafshnalten e Kurveleshit ne zonen Jonike. Bul. Shk. Gjeol. Nr. 1. Tirane. 

14. Serjani A., Bajo I., 1992 - Outcrops of Magmatic and Metamorphic rocks in the Ionian 

Zone (Albania). 6 th I. C. Athens. (IGCP 276, Newsletter Nr.6, 1998). 

15. Sulstarova E. 1987. Mekanizmi i vatrave te termeteve ne Shqiperi dhe fusha e sforcimeve 

tektonike te sotme. Bul. Shk. Gjeol. Nr. 4. Tirane. 

16. Shtreto Th., Xhufi Ç., Gjoka M. 1995. Some considerations on the hydrocarbon 

exploration in carbonate deposits in Ionian Zone. Proceedings: Current and Future 

Problems of oil industry in Albania. Fier. 

17. Tushaj D., Mehillka Ll., Xhufi Ç., Veizi V. 1991. Modeli strukturor i Albanideve te 

Jashtme. Bul. Shk. Gjeol. Nr. 1. Tirane. 

18. Velaj T., et al., 1999. Thrust Tectonics and the Role of Evaporites in American 

Association of Petroleum Geologists, Sept. 1999). 

177

178

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HYDROCARBON EVALUATION ASPECTS in MOLASSE RESERVOIRS, VLORË- 

ELBASAN REGION, ALBANIA 

Prof. Asc. Dr Vilson SILO * , Prof. Asc. Dr Kristaq MUSKA * , Eng. Erald SILO * 

*) Faculty of Geology and Mining, Tirana – ALBANIA 

The molasses deposits contain more than half of the reserves discovered in Albanian territory, 

from which more than 20 % are still undeveloped. The space interconnection of molasses 

deposits has brought to light the particularities of the geologic structure and given full view 

of the distribution of the reservoirs in close relation with their formation history. The 

paleorelief, mainly shelf, is made up of terraces, valleys and erosion uplifts and characterized 

by the transgression placement of molasses upon the limestone of the eroded structures of the 

continental border of the Ionian zone. Their regional connection has made possible the further 

improvements in the geologic structure and in the individualization of sedimentation 

environments. The organic matter present in them, and the condition and history of the 

geologic development have not been favorable to form the hydrocarbons. As a consequence, 

the oil is secondary, migrated from the limestone through direct contacts with them. Their oil 

and gas-bearingness is mainly related to lithological, lithologo-structural, bedded, tectonically 

screened and irregular reservoirs conditioned by the sedimentation environments. From the 

regional viewpoint, the deposits relate to the presence of bays, uplifts and erosion scales. The 

oil beds are concentrated in traps within the bays and outside, as a result of lithological 

changes that make possible their preservation. The reserves calculations made as now, 

evidencing the general potential of the molasses, have been based on the eastern 

classification, and been lacking from the economical viewpoint. Often, the analogy to the 

worldwide experience has been used. Under these conditions, in relation to reserves re- 

evaluation, the surfaces have been determined in accordance with the requirements of 

western classification into proven, probable and possible reserves increasing reliability. 

� 

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179

Attention has been paid in drawing the water-oil contacts where there have been variations by 

the change in the structural plane and reservoir re-formation. 

KEY WORDS: crude oil in the molasses deposits; the main migration ways are the 

transgressive contacts in Patos-Verbas, Kuçove and Selenica; in general, sandstone thickness 

increases from south to north and from east to west; 

REFERENCES 

1.- Dore, P., Silo, V., Thomai, L. 2005. “Presence of carbonate structures under throw of 

Kruja zone based on the seismic new data in Elbasani region, Albania”. Paper 

presented at the 4 th Congress of Balkan Geophysical Society, 9-12 October, Bucharest, 

Romania. 

2.- Dhimulla I. 1986. “Geochemical conditions of the oil and gas field formation in Albanian 

� 

territory”. National Scientific Center of Hydrocarbons Library, Fier, Albania. 

3.- Dhima, S., Prenjasi, E., Guri, S., Silo, V. 2002. “Complex geo-seismic study on thrusting 

tectonics and reflection of flysch folds at top limestone level in the Ionian zone”. Paper 

presented at the 3 -rd Balkan Geophysical Congress and Exhibition 24-28 June, Sofia, 

Bulgaria. 

4.- Gjoka M, Silo V, Sylari V, 2002 . “Geologic construction study of the oil and gas 

carbonate reservoirs in Albania”. National Scientific Center of Hydrocarbons Library, 

Fier, Albania. 

5.- Gjoka M, Ranxha S, Gjika A. 2002. “Geologic construction study and evaluation of the 

oil and gas reserves in Kreshpan-Kuçove regions”. National Scientific Center of 

Hydrocarbons Library, Fier, Albania. 

6.- Silo, V., Nishani, P., etc. 2006. “Seismic data contribution in prospecting carbonate 

structures of Ionian zone under of Kruja zone”. Paper presented at the International 

Scientific Symposium “Geo-Mining Potentials-Strategy and their Management”, 27-30 

September, Mitrovicë, Kosovo. 

7.- Silo, V., Nishani, P., Silo, E. 2008. “Hydrocarbon exploration under of Kruja zone in 

Tirana-Rodon area, Albania”. Paper presented at the 5 -th Congress of Balkan 

Geophysical Society, 5-8 October, Belgrade, Serbia. 

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180

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GAS DETECTION in the PERI-ADRIATIC DEPRESSION AREA by TRUE 

AMPLITUDE PROCESSING of SEISMIC DATA 

Prof. Asc. Dr. Vilson SILO * , Acad.Prof. Dr. Salvatore BUSHATI ** , Eng. Erald SILO * 

*) Faculty of Geology and Mining, Tirana – ALBANIA 

**) Academy of Sciences, Tirana – ALBANIA 

Gas potential is related in the Tortonian sandstone layers and the Miocene-Pliocene 

folded structures, as identified from the seismic data. Taking into consideration the 

dimensions of the prognosed structures in onshore, considerable reserves of biogenic 

and/or thermogenic gas are founded in this area. Based on processing seismic data, a 

new interpretation is accomplished to evaluate the possible gas bearing targets. An 

integrated lithological and seismic interpretation method has been used in a real case 

study of seismic amplitude anomalies (“bright spots”) related to shallow gas sands 

encased in shales. In this paper we give some aspects of true amplitude seismic data 

processing and seismic attributes for gas detection in some areas of Peri-Adriatic 

Depression. The results of this study calibrated on wells serve as guide lines in prospect 

evaluation whose expressions on conventional seismic sections are “bright spots”. 

Key Words: Gas fields, Gas potential, true amplitude seismic data processing, seismic 

attributes for gas detection, molasses sediments of the Peri-Adriatic Depression are 

terrigenous in origin and consist of clays and silts intercalated with sandstone beds. 

REFERENCES 

Denham, L., et al. 1985. The zero-offset stack. 55 th SEG Annual International Meeting, 

Washington, D.C.. 

Gary Yu., 1985. Offset amplitude variation and controlled amplitude processing. 

Geophysics, vol. 50. 

181

Hilterman, F.J., 1983. Seismic lithology: Continuing education course. 53 rd SEG 

Annual International Meeting, Las Vegas. 

Ostrander W. J., 1984. Plane wave reflection coefficients for gas sand at no normal 

angles of incidence. Geophysics, vol. 49. 

Rutherford S. R. and Williams R. H., 1989. Amplitude versus offset variations in gas 

sands. Geophysics, vol. 54. 

Silo V., 1994. True amplitude processing of seismic data for gas detection in Peri- 

Adriatic Depression area, Albania. PhD Thesis, Polytechnic University of Tirana, 

Department of Earth Sciences 

Silo V., 2004. Digital processing of seismic data used in petroleum exploration. 

Polytechnic University of Tirana, Department of Earth Sciences (Book for 

students) 

Shuey, R.T., 1985. A simplification of the Zoeppritz equations. Geophysics, vol. 50. 

Taner M. T., Koehler F. and Sheriff R. E., 1979. Complex seismic trace analysis. 

Geophysics, vol.. 44. 

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182




RECENT SEDIMENTS on VJOSA RIVER DELTAIC LITTORAL 

(Mineral composition and sedimentology) 

(POSTER) 

Agim SINOJMERI*, Çerçis DURMISHI*, Ana QORRI*, Eralda DAJA* and Erind 

ZAÇE* 

* Faculty of Geology and Mining: sinojmeri@yahoo.com 

The Delta of Vjosa River occupies a surface of 317 km 2 and forms a littoral of about 22 km. 

Following the combination of geological, tectonic, sedimentological as well as oceanographic 

processes, the Vjosa delta was displaced several time during the last century. 

The deposits of this delta are compiled mainly by sands, silty sands, clays and peat clays, but to 

the mouth of the river predominates sands and silty sands. To the littoral sediments, marine bars, 

beach ridges and dunes are present. Granulometry analysis reveals the fine granulometry of 

these deposits, where the curves morphology indicates a clear differentiation between dunes and 

beach deposits (Figure 1). 

Cumulative % 

100 

90 

80 

70 

60 

50 

40 

30 

20 

10 

0 

5/2/3 (beach) 

5/1/3 (dune) 

Silt 0.075 Sand 4.75 Gravel 

0.425 

0.01 0.1 1 10 

Grain dimensions (mm) 

Figure 1. Granulometric curves of beach sediments and dune from site 5 (Vjosa River delta). 

Considering the large variety of rock formations (ophiolites, molasses, limestones, flysch) 

leached by Vjosa River, the mineral composition of the deltaic sediments present large 

variations. 

Heavy mineral strata (Figure 2) up to 0.4m thick are observed in deltaic deposits of Vjosa River 

compiling marine placers. The heavy minerals constitute up to 60% of the bulk and are 

concentrated in thin intercalations, up to a few cm thick within these strata. 

0.2 mm 

Figure 3. Different shapes of 

garnets. Sample 4/1/3 

Rut 

Zr 

0.2 mm 

Figure 2. Different shapes and 

colors of zircon. Sample 

12/1/3

Figure 4. Heavy mineral strata in 

the southern part of 

Vjosa Delta 

Different mineral shape and colour indicate different origin of mineral sources. Besides 

chromite, which constitutes the majority of the heavy fraction of fine sandy deposits in Albania, 

in deltaic sediments of Vjosa is detected a large variety of garnets (Figure 3), different shape of 

zircon (Figure 4), different type of rutile, as well as traces of monazite and xenotine. 

Keywords: Beach sediments, Placer, Granulometry, Garnet morphology, Zircon morphology. 

REFERENCES 

Belousova E. A. Griffin W. L. and O’Reilly S. Y., 2006. Zircon crystal morphology, trace 

element signature and Hf isotope composition as a tool for petrogenetic modeling: 

Example from Eastern Australian granitoids. Journal of Petrology, 47, 329-353. 

Durmishi Ç., 1997. Bazat e sedimentologjisë. SHBLU, Tiranë. 

Durmishi.Ç, Beshku H. et al., 2002-2005. Studimi gjeologo sedimentologjik dhe monitorimi i 

hapesires bregdetare te Shqiperise -impaktet ne zhvillimin mjedisor, infrastrukturor ,urban 

dhe turistik. Fondi i SH.GJ.SH. Tirane. 

Ricci Lucchi F., 1980. Sedimentologia. CLUEB. 

Sinojmeri A., 2006. Kristalografia dhe kristalokimia në këndvështrimin e gjeologut. SHBLU 

Tiranë. 

Trushkova N. N. and Kuharenko A.A., 1961. Atlas of placer minerals. VSEGEI. 

184




SEDIMENTOLOGY, DIAGENESIS and FRACTURING HISTORY 

of the UPPER CRETACEOUS LIMESTONES in the IONIAN ZONE 

(CENTRAL and SOUTHERN ALBANIA). 

Rudy Swennen 

Earth and Environmental Sciences 

K.U.Leuven, Celestijnenlaan 200E 

B-3001 Heverlee-Leuven, Belgium 

Rudy.Swennen@ees.kuleuven.be 

Several of the oil fields in Central and Southern Albania are situated in Upper Cretaceous 

deep marine limestone turbidites and debris flows. Due to the fold- and thrust nature of the 

external Albanides several reservoir analogue structures are well exposed in the field 

(Saranda, Kremenara, …). Based on a regional study using crosscutting relationships 

between diagenetic phases (cements, stylolites, veins, reactivated fractures, …) it was possible 

to reconstruct the diagenetic history and to define the diagenetic stages that exert a major 

control on the reservoir properties of these deep marine limestones (Van Geet et al., 2002). 

A first important, pre-compactional stage relates to marine burial diagenesis, whereby a 

selective cementation of the turbidite matrix is of importance. The amount of ideal nucleation 

sites such as rudist debris seems to control the degree of cementation and subsequent burial 

compaction, explaining the existence of tight and porous (oil impregnated) lithologies 

(Dewever et al., 2007). A major (initial) porosity destructive process relates to the 

development of burial stylolites as well as tectonic stylolites. Notice, however, that in some 

areas these stylolites became reactivated and some secondary porosity development has been 

recognised. Based on the crosscutting relationship with calcite cemented veins, a set of preburial 

stylolitisation veins, a set of post- burial but pre-tectonic stylolitisation veins, and a set 

of post- tectonic stylolitisation veins can be differentiated, whereby only in the last set of 

veins indications of the involvement of non-host rock buffered fluids can be inferred based on 

the ferroan nature of some of the vein infill as well as the existence of dolomite and fluorite 

infill phases (Vilasi et al., 2009). Another important diagenetic event is a karstification event, 

related to the fore-budge development of some of the anticlinal structures during fold- and 

thrust development. These karsts are however often difficult to recognise. Of major 

importance with regard to reservoir development is the reactivation of some of the veins, and 

thus its reopening. It is especially along these veins that major oil seepage in the field can be 

seen. The latter may relate to the Miocene reactivation of some of the tectonic movements as 

testified the onlapping transgressive conglomerates that now occur as inclined as well as 

vertical beds in some of the studied outcrops (Breesch et al., 2007). Noteworthy is the 

development of a second set of burial stylolites post-dating conglomerate deposition, 

indicating that some deformed areas underwent a rather important second burial. 

Reconstruction of the diagenetic history in field analogues is undoubtly a powerful tool to 

better understand the control on reservoir performance in Upper Cretaceous deep marine 

limestones in Central and Southern Albania as well as in the Adriatic Sea. 

185

References 

Breesch, L., Swennen, R., Dewever, B. and Mezini, A., 2007, Deposition and diagenesis of 

carbonate conglomerates in the Kremenara anticline, Albania: a paragenetic time marker 

in the Albanian foreland fold-and-thrust belt, Sedimentology, 54, 483-496, doi: 

10.1111/j.1365-3091.2006.00835.x. 

Dewever, B., Breesch, L., Swennen, R. and Roure, F., 2007, Sedimentological and marine 

eogenetic control on porosity distribution in Upper Cretaceous carbonate turbidites 

(central Albania), Sedimentology, 54, 243-264, doi: 10.1111/j.1365-3091.2006.00833.x. 

Van Geet, M., Swennen, R., Durmishi, C. and Roure, F., 2002, Paragenesis of Cretaceous to 

Eocene carbonate reservoirs in the Ionian fold and thrust belt (Albania): relation 

between tectonism and fluid flow. Sedimentology, 49, 697-718. 

Vilasi, N., Malandain, J., Barrier, L., Callot J.P., Amrouch, K., Guilhaumou, N., Lacombe, O., 

Muskha, K., Roure, F. and Swennen, R., 2009, From outcrop and petrographic studies to 

basin-scale fluid flow modelling: the use of the Albanian natural laboratory for 

carbonate reservoir characterisation. Tectonophysics, 474, 367- 

392.doi:10.1016/j.tecto.2009.01.033. 

186




GEOCHEMICAL CONSTRAINTS (Nd, Pb ISOTOPE RATIOS and TRACE 

ELEMENTS) on the MESOZOIC VOLCANISM in ALBANIA 

Artan TASHKO 1 & Georges H. MASCLE 2 

1 Polytechnic University of Tirana, Rruga Elbasanit,355, 1001, Tirana, Albania. 

2 Laboratoire de Géodynamique des Chaînes Alpines. Université Joseph Fourier (UJF), 

Maison des Géosciences, BP 53, 38041 Grenoble Cedex, France 

e-mail:tashkoar@gmail.com 

Keywords: Nd and Pb isotopes, trace elements, volcanic rocks, geochemistry, Albania. 

Three phases of the Mesozoic geodynamic evolution in Albanides can be distinguished, based 

on the geochemical characteristics of the volcanic rocks. 

1. A rifting phase of the Early Triassic (Permian -Triassic?) to Middle Triassic. 2. Spreading 

phase of the Middle Triassic to Middle Jurassic and 3. A new spreading phase of the Middle 

Jurassic. 

During the Early Triassic volcanic rocks were formed, derived from an enriched mantle 

source (EMII) in the continental rifting phase. These volcanic rocks are characterized by 

negative �Nd values (-1.91), high Th, Zr and REE (20–100 times chondrites) content and 

marked negative Eu, Ti and Nb-Ta anomalies. 

Some Middle Triassic volcanic rocks are characterized by low �Nd values (+0.69 to +1.98), 

high Zr and REE (3–20 time chondrites) content, but by a very low Th content and no marked 

Eu and Nb-Ta negative anomalies. The magma source is an enriched mantle of type EMI. For 

all these volcanic rocks of the first group (samples G13,G9,G11and G6) crust contamination 

component is evident from the low �Nd values and the fractionation of REE, LREE being 

clearly enriched compared to HREE. 

Subsequently, in the spreading phase, the oceanic crust evolved to the basalts of the volcanosedimentary 

series (T2-J1), characterized by higher �Ndi values, ranging from +6.5 to +7.7, a 

REE content about 10 times chondrites, flat REE patterns to LREE depleted, no Nb-Ta 

negative anomalies, low Th contents (0.2 ppm, on average) and a relatively high (1.3 %) 

TiO2 content. These basalts series (G1, G2, G8, G10, G12, G14, G15, and G16 samples) were 

probably formed in an opening of a back-arc basin context (BABBs) from a depleted mantle 

magma source (DM). The same magma source produces the basalts of Jurassic western 

ophiolite type (J2 basaltic series, sample G7) that have the same geochemical characteristics as 

the basalts of the volcano-sedimentary series. 

Jurassic volcanic rocks of the eastern ophiolite type (J2 basalt-andesitic series, samples G3 and 

G4) show the same geodynamic conditions (i.e. BABBs) but have a distinctively different and 

more depleted magma source (DMM) as evidenced by the lower REE, Ti and Zr content, 

though, the �Ndi values (+5.58 to +6.94) are quite similar. Significantly lower-than-chondrite 

Zr/Hf radios may be explained by a previous zircon fractionation, as zircon mineral is the 

primary reservoir for both Zr and Hf and preferentially incorporates Zr. 

187

The Pb isotope ratios of all rocks studied do not testify to the existence of an HIMU 

component in the magma source. The observed trend, from OIB volcanism in the southern 

part of the Eastern Mediterranean (Cyprus) to back-arc basin basalts associated with arcrelated 

and with in-plate volcanism in the northern part (Greece), seems to evolve in Albania 

with a decreasing role of oceanic within-plate volcanism (enrichment by HIMU source). 

Figure 1: Chondrite-normalized REE compositions (normalization values after Sun and 

McDonough,1989). Dashed lines contour the field of the Triassic volcano-sedimentary 

series (G10 was the representative sample of this series). 

188

Figure 2: Extended multi-element variation plots normalized to primitive mantle 

(normalization values after Hoffman, 1988) 

189

Figure 3: Th/Yb versus Ta/Yb plot. Fields, after Pearce1983. 

Figure 4: Plot of �Ndi vs. 206 Pb/ 204 Pbi for selected volcanics. Isotopic reservoirs after Zingler, 

and Hart (1986). Samples OT-5, OT-7 and OT-17 from Othrys , respectively OIB alkali basalt, BABB 

and IAT after Monjoie et al.,2008. Sample CY02 from Cyprus alkali basalts ( Lapierre et al. ,2007). 

190

REFERENCES 

1. Lapierre 

H., Bosch D., Narros A., Mascle G.H., Tardy M. & Demant A. The mamonia 

complex revisited: remnants of late Triassic intra-oceanic 

volcanism along the Tethyan 

southwestern passive margin. Geol. Mag., 144, 2007, 1–19. 

2. Monjoie 

Philippe, Henriette Lapierre, Artan Tashko, Georges H. Mascle, Aline Dechamp, 

Bardhyl Muceku, and Pierre Brunet. Nature and origin of the Triassic volcanism in Albania 

and Othrys: a key to understanding the Neotethys 

opening? Bulletin de la Societe Geologique de 

France, Jul 2008; 179, 2008: 411 – 425. 

3. Pearce 

J. A. Role of the sub-continental lithosphere in magma genesis at active continental 

margin.In Hawkesworth C. J. & Norry 

M. J. (eds). Continental Basalts and Mantle Xenoliths, 

1983, pp. 230–49. Shiva, Nantwich. 

4. Sun, 

S.S. and McDonough, W.F., Chemical and isotopic systematics of ocean basalts: 

implications for the mantle composition and processes. In: Saunders, A.D., Norry, M.J. (Eds). 

Magmatism in the ocean basins. Geol. Soc. London Spec. Publ., 42, 1989, 313–345. 

5. Zingler, 

A. and Hart, S.R., Chemical geodynamics. Ann. Rev. Earth Planet. Sci., 14, 1986, 493. 

191

192




Strength and weakness of the World lithosphere 

Magdala Tesauro (1), Mikhail K. Kaban (1), Sierd A.P.L Cloetingh (2) 

(1) GeoForschungsZentrum Potsdam (GFZ), Germany (2) VU University, The Netherlands, 

magdala@gfz-potsdam.de, kaban@gfz.potsdam.de, sierd.cloetingh@falw.vu.nl 

Rheology and strength of the Earth’s lithosphere have been debated since the beginning of the 

last century, when the concept of a strong lithosphere overlying viscous asthenosphere was 

introduced. The issue of strength of the lithospheric plates and their spatial and temporal 

variations is important for many geodynamic applications. For rocks with given mineralogical 

composition and microstructure, temperature is one of the most important parameters 

controlling rheology. We present the first world strength map obtained from global crustal 

(Fig.1a) and thermal models (Fig. 1b). Temperature estimates for the deeper horizons of the 

lithosphere, where the heat transport is mostly conductive, requires a precise knowledge of 

many crustal parameters (mainly thermal conductivity and heat production), which are 

extremely uncertain. Therefore, we use a combination of indirect approaches, such as seismic 

tomography and geothermal analysis (Ritsema and Van Hejist, 2004 ; � ermák, 1993). 

Furthermore, we implement a global crustal model by assembling the most recent 

compilations (e.g. Mooney and Kaban, 2010 ; Tesauro et al., 2008). Rheology of the upper 

and lower crust (Fig.1c) was classified based on a tectonic maps of the World (Mooney, 

2009). The results show a good correspondence between strength values and geological 

features (Fig. 2). Pronounced strength contrasts exist between old cratons and areas affected 

by the Tertiary volcanism, which are mostly coincident with the boundaries of seimogenic 

zones. The Te in the continents (Fig. 3) demonstrates a bimodal distribution around two peaks 

at ~25 km, which is the representative value for the continental areas outside of the cratons, 

and at ~70 km, which is a common value for the cratons. This clustering is probably related to 

influence of the plate structure: depending on the ductile strength of the lower crust, the 

continental crust can be mechanically coupled or decoupled with the mantle resulting in 

highly different Te values. The largest changes of Te occur at sutures that separate different 

provinces characterized by major changes in the lithospheric strength. The lithosphere 

strength appears to be primary controlled by the crust in the young (Phanerozoic) geological 

provinces characterized by low Te (~25 km), high topography (>1000m) and seismicity. By 

contrast, the old (Achaean and Proterozoic) cratons of the continental plates show high Te 

(over 100 km), low topography (

References 

� ermák, V., 1993. Lithospheric thermal regimes in Europe. Phys. Earth Planet. Int., 79, 179-193. 

Ritsema, J., van Heijst, H., 2004.Global transition zone tomography. J. Geophys. Res, 109, B02302, 

doi:10.1029/2003JB002610. 

Mooney, W.D., 2009. in: Treatise on Geophysics, B. Romanowicz, A. Dziewonski, G. Schubert, Eds. 

(Elsevier, Amsterdam, NL), Vol. 1, Chap. 11, pp.361-417. 

Mooney, W., Kaban, K., 2010. The North American Upper Mantle: Density, Composition, and 

Evolution,J. Geophys. Res. (in print). 

Tesauro, M., Kaban, M.K, .Cloetingh, S.A.P.L., 2008. EuCRUST-07: A new reference model for the 

European crust. Geophys. Res. Lett. 35, LXXXXX doi:10.1029/2007GL032244. 

Tesauro, M., Kaban, M.K., Cloetingh, S.A.P.L., 2009. A new thermal and rheological model of the 

European lithosphere. Tectonophysics, 476, 478-495. 

194

Fig. 1 (a) Moho depth, (b) Temperature (C˚) at 100 km depth, (c), Global Rheology Map of the 

Upper and Lower crust. Numbers stand as follows: 1, Granite-Mafic garnet granulite, 2, Granite- 

Diabase, 3, Quarzite-Diabase, 4, Quarzite-Diorite, 5, Diabase. 

195

Fig. 2 Integrated Strength of the lithosphere estimated for compressional conditions (Pa m). 

Fig. 3 Lithospheric Elastic Thickness (Te). 

196




CHARACTERIZATION of the FLUID FLOW in the ALBANIDES FORELAND 

FOLD-and-THRUST BELT (SOUTHERN ALBANIA) 

Nadège VILASI 1 , Jean-Paul CALLOT 2 , Francois ROURE 2 , and Rudy SWENNEN 3 

1 Statoil ASA, Stavanger NORWAY 

2 IFP Energies Nouvelles, Rueil-Malmaison France 

3 Katholieke Universiteit Leuven BELGIUM 

Albania displays a unique petroliferous foreland fold-and-thrust belt system. It corresponds to 

a complex tectonic assemblage, made up of thin-skinned allochthonous units, progressively 

emplaced during the Neogene deformations. The continuous Oligocene to Plio-Quaternary 

sedimentary records help to constrain both the burial history of Mesozoic carbonate 

reservoirs, the timing of their deformation, and the coupled fluid flow and diagenetic 

scenarios. 

The integration of the interactions between petrographic and microtectonic studies, kinematic, 

thermal and fluid flow basin modelling, has been studied in detail. The fracturing of the 

reservoir intervals has a pre-folding origin and relates to the regional flexuring in the foreland. 

The first recorded cement has a meteoric origin, implying downward migration and the 

development of an earlier forebulge in the Ionian Basin. This fluid, which precipitates at a 

maximum depth of 1.5 km, is highly enriched in strontium, attesting for important fluid–rock 

interaction with the Triassic evaporites, located in diapirs. From this stage, the horizontal 

tectonic compression increases and the majority of the fluid migrated under high pressure, 

characterised by brecciated and crack-seal vein. The tectonic burial increased due to the 

overthrusting, that is pointed out by the increase of the precipitation temperature of the 

cements. Afterwards, up- or downward migration of SO4 2� , Ba 2+ and Mg 2+ -rich fluids, which 

migrated probably along the décollement level, allows a precipitation in thermal 

disequilibrium. This period corresponds to the onset of the thrusting in the Ionian Zone. The 

last stage characterised the uplift of the Berati belt, developing a selective karstification due 

likely to the circulation of meteoric fluid. 

The fluid flow modelling allowed to reconstruct the hydrocarbon generation and migration 

but also to trace the changes in the water flow through time (origin, migration pathways and 

velocity). The third utility consists of determining the evolution of the overpressuring periods 

through time and space and then to correlate them to the overpressuring periods determined 

by studying the fracture-fillings. This will help to place the diagenetic evolution in the 

tectonic evolution of the FTB. The main results of the hydrocarbon fluid flow modelling show 

that the Upper Cretaceous-Eocene carbonate reservoirs in the Ionian zone have been charged 

from the Tortonian onward, and that meteoric fluid migration should have intensely 

biodegraded the hydrocarbon in place. Concerning the migration paths, it has been 

demonstrated that the thrusts act principally as flow barriers in Albania, mainly due the 

occurrence of evaporites (non-permeable), except in the foreland, where they do not occur. 

The results of the modelling demonstrate that the water migrations are dominantly vertical 

197

during the flexure of the foreland. Then the increase of the sedimentary overburden and the 

thrusting of the units imply upward water migration under high pore fluid pressure. The 

development of a high topographic relief caused large downward and lateral meteoric fluid 

flow, which is characterised by higher velocities. From the thrusting phase onward, the faults 

act as flow barriers, due to the occurrence of evaporites along the décollement levels and 

compartmentalise the reservoir interval. 

198




SCOPSCO: SCIENTIFIC COLLABORATION on PAST SPECIATION CONDITIONS 

in LAKE OHRID (ALBANIA/MACEDONIA) – towards an ICDP DEEP DRILLING 

Hendrik VOGEL 1 , B. WAGNER 1 , T. WILKE 2 , A. GRAZHDANI 3 , G. KOSTOSKI 4 , S. 

KRASTEL 5 , K. REICHERTER 6 , G. ZANCHETTA 7 

1 

University of Cologne, Institute of Geology and Mineralogy, Cologne, Germany 

(vogelh@uni-koeln.de; wagnerb@uni-koeln.de) 

2 

Institute of Animal Ecology and Systematics, Justus Liebig University Giessen, Germany 

3 

Universiteti Politeknik, Fakulteti i Gjeologjise dhe Minierave, Tirane, Albania 

4 

Hydrobiological Institute Ohrid, Republic of Macedonia 

5 

Institute Cluster of Excellence: The Future Ocean, Leibniz Institute of Marine Sciences 

(IFM-GEOMAR), Kiel, Germany 

6 

Institute of Neotectonics and Natural Hazards, RWTH Aachen University, Germany 

7 

Dipartimento di Scienze della Terra, Università di Pisa, Italy 

Lake Ohrid is a transboundary lake with approximately two thirds of its surface area 

belonging to the Former Yugoslav Republic of Macedonia and about one third belonging to 

the Republic of Albania. With more than 210 endemic species described, the lake is a unique 

aquatic ecosystem and a hotspot of biodiversity. This importance was emphasized, when the 

lake was declared a UNESCO World Heritage Site in 1979, and included as a target area of 

the International Continental Scientific Drilling Program (ICDP) already in 1993. Though the 

lake is considered to be the oldest, continuously existing lake in Europe, the age and the 

origin of Lake Ohrid are not completely unravelled to date. Age estimations vary between one 

and ten million years and concentrate around two to five million years, and both marine and 

limnic origin is proposed. 

Extant sedimentary records from Lake Ohrid cover the last glacial/interglacial cycle and 

reveal that Lake Ohrid is a valuable archive of volcanic ash dispersal and climate change in 

the central northern Mediterranean region. These records, however, are too short to provide 

information about the age and origin of the lake and to unravel the mechanisms controlling 

the evolutionary development leading to the extraordinary high degree of endemism. 

Concurrent genetic brakes in several invertebrate groups indicate that major geological and/or 

environmental events must have shaped the evolutionary history of endemic faunal elements 

in Lake Ohrid. High-resolution hydroacoustic profiles (INNOMAR SES-96 light and 

INNOMAR SES-2000 compact) taken between 2004 and 2008, and multichannel seismic 

(Mini-GI-Gun) studies in 2007 and 2008 demonstrate well the interplay between 

sedimentation and active tectonics and impressively prove the potential of Lake Ohrid for an 

ICDP drilling campaign. The maximal sediment thickness is ˜680 m in the central basin, 

where unconformities or erosional features are absent. Thus the complete history of the lake is 

likely recorded. A deep drilling in Lake Ohrid would help 

(i) to obtain more precise information about the age and origin of the lake, 

(ii) to unravel the seismotectonic history of the lake area including effects of major 

earthquakes and associated mass wasting events, 

199

(iii) to obtain a continuous record containing information on volcanic activities and climate 

changes in the central northern Mediterranean region, and 

(iv) to better understand the impact of major geological/environmental events on general 

evolutionary patterns and shaping an extraordinary degree of endemic biodiversity as a matter 

of global significance. 

For this purpose, five primary drill sites were selected based on the results obtained from 

sedimentological studies, tectonic mapping in the catchment and detailed seismic surveys 

conducted between 2004 and 2008. For the recovery of up to ca. 680 m long sediment 

sequences at water depths of more than 260 m a newly developed platform operated by 

DOSECC shall be used. The drilling operation is planned to take place in 2011. 

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