taste oil and wine

Taste Oil and Wine – Field Trip

CONTENTS

INVITATION pg. 1

HADES VS. GEOLOGY

General Geological Setting pg. 2

Moldavides Basin - geological setting pg. 6

Oligocene- Early Miocene – Kliwa Facies – Details pg. 8

Foredeep – Geological Seetting pg. 10

Hydrocarbon Fields in the Eastern Carpathians pg. 12

HADES VS. OILMANS (THE TASTE OF OIL)

Field Trip itinerary pg. 14

“Taste Oil and Wine” Field trip Timetable pg.14

Stop descriptions pg 15

Stop 1 - Berca – Arbanasi Oilfield – Mudy Volcanoes pg 15

Stop 2 – Valea Rea (Chirilesti) – Kliwa Sandstone Outcrop Pg.18

Stop 3 – Valenii de Munte – Free Time pg. 21

Stop 4 – National Oil Museum – Ploiesti pg. 23

Stop 5 Boldesti Oilfield – Seciu pg. 26

DIONISOS VS. OILMANS (THE TASTE OF WINE)

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INVITATION

You may wonder what the connection would be between the Oil and the Wine.The Oil and the Wine are liquids of the earth generated in time (Chronos); the older they

are, the better they become. The former comes from the very kingdom of Hades (the master of the riches and the god of the underground realm); the other one coming from his uncle, Dionysus (the protector god of the vine-growers).

Therefore, there is no wonder that the Curvature Sub-Carpathians hills covered by vineyards contain oil in the earth bowls. That is why we suggest to you a trip across these regions in a unique combination; to the spectacular kingdom of Hades and in Dionysus’ magnificent wine world.

And if you are indeed oil men, you have had at least once the occasion of washing away with a healthy mug of wine, the taste and smell of oil, deeply penetrated in your bowels, after dayin, day out operations and works conducted in the wells.

Of course, a mug of wine can be a way of success cheering or drowing a failure, in any of the activity fields connected to oil and not only… But to enjoy a mug of wine as an oilman means a particular balance between sulphur alcohols and “pinot noir” or between brimstone and “riesling”.

The trip we suggest to you is a test. If you feel very well in both the kingdom of Hades and in the one of Dionysus, it means you are oil men, or you can become oil men. If not, it means that it is likely you have gone astray…

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HADES VS. GEOLOGY

GENERAL GEOLOGICAL SETTING

Romania's territory, which belongs to the geological structural ensemble of central and south-eastern Europe, consists of a chain segments from the Alpidic Pericratonic Belt of the Carpathians-Balkans-Rhodopes-Pontides, from the Alpine Intercratonic Belt North Dobrudja - South Crimeea the Great Caucasus, as well as from their Foreland represented by the East-European Platform, the Central European (Scythian) Platform and the Moesian Platform. The last two platforms and their intercratonic chain also extend on to the Black Sea Continental Shelf.

Fig. 1 The main geotectonic units of Romania, after Sandulescu, 1984, in Ciulavu, 2000

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Taste Oil and Wine – Field TripCarpathians represent an arched orogene, having a complex structure wherein the flysch

nappes modify their trend with 200 from the northernmost area (Poland) down to the south, in the curvature zone of Romania.

The segment of the Alpine belt comprised between the Tisza springs in the north and Dambovita Valley in the south represents the the Romanian Eastern Carpathians. This orogene is continued with Ukraina’s Eastern Carpathians to the north and southwards with the Southern Carpathians.

The geotectonic units that border the Eastern Carpathians are: to the east, up to Bistritei Fault, the East European Platform, with a Precambrian basement, known across the Romanian territory under the name of the Moldavian Platform; to the south and east (to the south of Bistrita Fault) the Paleozoic Platform, consisting of two segments separated by the transcrustal Peceneaga –Camena Fault, one of the segments being called the Scythian Platform and the other one, the Moesian Platform to the south-west; to the west the Transylvanian Basin, a post-tectonic depression (Fig. 1).

Săndulescu (1988) divides the Alpine history of the Carpathian area into an extensional Triassic-Neocomian period followed by a compressional Neocomian – Miocene one.

The Alpine geotectonical evolution of the Carpathians kicked off by setting in two expansion zones: an oceanic rift, with passive continental margins (Atlantic type) and an intracontinental rift (Afar-Red Sea type) located to the east as compared to the former. This distension period developed during the Middle Triassic – Lower Cretaceous interval. The oceanic rift got unconfined in the Lower Triassic, whereas the intracontinental one in the Lower Jurassic, the two rifts evolving in an expansion regime till the Upper Jurassic (the oceanic one) and respectively the Lower Cretaceous (the intracontinental one). Since the Lower Cretaceous (Barremian), the direction of the movements is changed, setting in a compression regime in both basins.

Depending on the intensity of the deformations, two major compression periods could be distinguished, which generally affected different orogenic areals: Dacidic period, characterized by two deformational paroxysms (MesoCretaceous and Late Cretaceous) and the Moldavian period, generally Miocene, but also within it, recognizing three tectogenetic phases. The two compression periods are responsible for setting up melting paleoplanes, oceanic and/or continental crust shields and tectonic “nappes” structuring.

The tectonic units involved in the evolutive model presented, partially can also be recognized in the actual structure of the Eastern Carpathians (Fig. 2, 3). Thus, the oceanic suture of the western basin was structured in the Transylvanian nappes obducted over the Median Dacides which constituted the eastern continental margin of the oceanic rift and were bordered to the east by the intracontinental rift. These two units, Transylvanian Nappes and Median Dacides, make up in a classical way the Crystalline-Mesozoic Area of the Eastern Carpathians, and the post-tectonogenic cover of the Median Dacides was associated to the TransCarpathian Flysch zone, along with the Piennides (nappes represented by oceanic sediments). The intracontinental suture is found in the External Dacides (underthrust and partially melted through subduction processes) together with a part of the geosynclinal fill folded during the Dacidic compression period, the remaining deposits in the intracontinental basin were thrust during the Miocene compression period, making up the Moldavides unit. The External Dacides together with the Moldavides are also known under the name of Flysch Zone, divided into the Inner Flysch and Outer Flysch. The crust melting within the intracontinental basin, generated, through subduction onto a melting paleoplane dipping westwards, Neogene-Lower Quaternary volcanic products, known under the name of the Neogene Volcanites Zone.

The Eastern Carpathians are characterized by the geosynclinal polarity typical to the Alpine orogenes. Thus, it is worth noticing a structural polarity expressed through the eastward vergent of the major units and an orogenic polarity given by the migration during the folding, from old to

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Taste Oil and Wine – Field Tripyoung and from inside (west) to outside (east). At the same time and in the same way, the depocenter of the sedimentary basin also migrated. This polarity is responsible for a remarkable cross-zonation. From outside to inside, the Subcarpathian Zone, the Flysch Zone and the Crystalline-Mesozoic Zone are distinguished.

As far as the oil generation and accumulation potential is concerned, only the Moldavides and respectively the Foredeep in front of this assemblage present a remarkable interest. This is the reason why we will focus our attention on them.

Fig. 2 Geotectonic structure of the Eastern Carpathians, after Bădescu, 1999

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Fig. 3 Nomenclatures and geostructural equivalencies in the External Dacides and Moldavides

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MOLDAVIDES BASIN - GEOLOGICAL SETTING

The term of Moldavides was introduced to designate the tectonic units which make up the Eastern Carpathians’ external flysch and molasse. The Moldavides complex is a succession of N-S trending imbricated thrust nappes and which consist of Cretaceous-Tertiary sedimentary rocks. The oldest nappes of the complex consist of Cretaceous rocks and lie in the westernmost part (inner). The nappes of the Moldavidic complex are (W-E; fig 4): i) Teleajen (Curvicortical), Macla and Audia – all consisting of Cretaceous rocks; ii) Tarcău and Marginal Folds (Vrancea) – they consist of both Cretaceous and Tertiary rocks; iii) Subcarpathian exclusively consisting of Tertiary rocks. The sedimentary basin, herein called the Moldavides Basin, was characterized by either the oceanic crust or thinned continental crust which, in the end, was subducted underneath Tisia-Dacia Block (Zweigel et al. 1998).

Fig 4. Skematic geological section in central part of Eastern Carpathians (in Maţenco and Bertotti, 2000).

The Moldavides Basin has the evolution characteristic to a remnant oceanic basin which was flanked at the inner part by a convergent margin and wherein the sedimentation had a strong turbiditic character. The term of remnant oceanic basin is quite general and denotes that the basin was sequential narrowed progressively due to tectonic events (Ingersoll et al., 1995). The basin’s main source areas were placed in the orogene (Anastasiu, 1984 and 1992) and supplied sediment at a rate which was increasing concurrently with the basin narrowing due to the rather continuous convergence. The high sedimentation rates and the stong subsidence are mirrored nowadays in the large thicknesses (thousands of metres) of the rock-stacks (Săndulescu, 1984; Mutihac, 1990) which make up the tectonic units (nappes) of the Moldavides. Most of the facies in the Moldavidic units lying within the Cretaceous – Eocene interval (Oligocene1) are characteristic to depositional deep sea-turbiditic (Contescu, 1974), hemipelagic or even pelagic environments. The flexural loading (Maţenco et. al, 1997) of the basin determined the formation of one (or even more?) basin(s) of peripheric foreland (sensu Miall, 1995) beginning with the uppermost Oligocene through Miocene. Thus, a great facies change is especially noticed on the eastern basin margin, where shallow marine facies (which occur within Kliwa-type lithofacies) are followed in a stratigraphic succession (Miocene) by continental and transitional facies.

The compressional deformations (fig. 5) began with the Lower Miocene (Lower Burdigalian), concurrently with thrusting the Curvicortical Flysch/Audia Nappes, followed by shortening along approx.E-W trend (Upper Burdigalian). The effect thereof resided in thrusting the Tarcău Nappes, the Marginal Folds as well as the inner part of the Subcarpathian Nappe. A second shortening took place in the Sarmatian and led to Subcarpathian Nappe thrusting over the non-deformed foredeep as well as the deformation of the post-Burdigalian sequences deposited over the Tarcau and Marginal Folds Nappes domain.

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Taste Oil and Wine – Field TripThe next deformational stage (Upper Miocene: Upper Sarmatian- Lower Meotian) was

characterized by a regime of compressional strike-slip movements along NNE-SSW to N-S trend. To the N, beyond Trotuş Fault, the strike-slip deformations were taken over by E-W sinistral faults, whereas, in the South of the Eastern Carpathians by NW-SE dextral faults. The transition zone underwent a shift towards ESE, estimated to 40-50 Km, (Maţenco and Bertotti, 2000).

Along the Pliocene-Pleistocene interval, the curvature area experienced thusting processes accompanied by shortening along NNW-SSE trend (Hippolyte and Săndulescu, 1996), of approx. 22 km. (Roure et al., 1993) or 15 km (Maţenco and Bertotti, 2000). While Roure et al., (1993) suggest that the shortening also involved the basement, Maţenco and Beetotti, (2000), consider that only the sedimentary cover was deformed.

The significant uplifts recorded throughout the Upper Badenian – Lower Sarmatian interval, in the central area of the Eastern Carpathians, resulted in the erosion of an approx. 5 km sedimentary stack.

The main uplifted area in the curvature zone is younger and it began with the Upper Miocene (Pontian), coeval with the youngest compressional moments (Sanders et al, 1999).

Fig. 5 Stratigraphic columns in the external Moldavides units and the main tectonic events (Maţenco and Bertotti, 2000)

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Oligocene- Early Miocene – Kliwa Facies - Details

The Oligocene deposits are found as three distinct lithofacies (Fusaru, Moldovita and Kliwa- Stefanescu, 1986); they succeed from the west to the east, and show sensitive longitudinal facies variations, from the Suceava Valley up to the Teleajen Valley.

Kliwa Sandstone Facies and Bituminous Facies (1500 m) lies in the eastern part of the TN and in MFN. It is characterized by the Kliwa-type quartz-SS. In lithostratigraphic succession comprise several entities, as follows (Fig 6):

- Gray slates (100-200 m thick);- Lower menilite sequence (20-30 m) with marls, shally clays and menilites;- Bituminous marls sequence with menilite interbeds (100 m);- Lower dysodilic shale sequence (200 m) with centimetric interlayers of quartz-

sandstones;- Kliwa quartz-sandstone sequence (600-1000 m) - individualized as an unit in the

northern area of the TN, and as two distinct horizons: “Lower Kliwa” and “Upper Kliwa” (in places bituminous and, in that case, an equivalent of the “Bustenari Sandstone”) - separated by the “Podu Morii Beds”. Frequently, the decimetric and metric units of quartz-sandstones alternate with decimetric and centimetric levels of the bituminous or dysodilic shales;

- Podu Morii Beds (80-200 m; Lower Miocene) constitute rhythmically clayey sandy flysch sequences with interbeded "tuff"; it represent a lateral variation of the Vinetisu Facies;

- Upper Dysodile and Menilite facies (120-140 m) outcrops in MFN and comprises 2 units as follows:

- Upper Dysodile sequence (100-120 m) consisting of dm-m units thinly- laminated (dysodilic) shale alternating with cm-dm units of quartz - sandstone;

- Upper Menilite sequence (10-20 m) constituted from menilites (2-5 cm in thickness) alternating with dysodilic shale and thin layers of quartz sandstones.

In places the above- mentioned sequences are found associated with diatomite. The age is probably Lower Miocene.

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Fig 6. Sedimentary Formations of the Moldavides

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FOREDEEP – GEOLOGICAL SETTING

In the acceptance of the Romanian geologist, only the formations younger than the last tectonogenesis of the Moldavides, namely Neosarmatian – Pleistocene molasses, were assigned to the Foredeep (Sandulescu et al. 1981; Sandulescu, 1894).

In this acceptance, the Foredeep (s.str.) was divided in two zones: an unfolded and a folded one.

The Unfolded Foredeep is superposed on the Foreland units. South of the Trotus Valey a narrow strip of the inner limb of the unfolded Foredeep overlaps the front of the Subcarpathian Nappe. The most typical sector of the unfolded Foredeep is the so-called “Focsani Depression”, of lop-sided shape and filled with thick molasse sediments (more than 10 km in the central part). Northwards and south-westwards, in the axial trend, it gets narrower and has a reduced thickness.

Inside the Focsani Depression the molasse formations show a monotonous lithology: mostly sandy molasses with andesitic sinerite layers at the Kersonian / Meotian boundary and richer in gravels. In the Upper Pliocene – Pleistocene, coals are also known.

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Fig 7. Folded Foredeep – Synthetic Litho-stratigraphic Column

Taste Oil and Wine – Field TripThe folded Foredeep deposits are developed in the Bend Area (“Diapiric Folds Zone”),

where, as mentioned before, they overlay the Subcarpathian Nappe and partialy, the outer marginof the Tarcau Nappe. A more diversified lithology is known here (excepting the molasse, neritic limestones in Kersonian, Schlier facies in Pontian, etc.) In this area, the Upper Sarmatian – Pliocene arenitic sequences proved to be the most important for the existence of oil and gas fields discovered so far.

The folding of this part of the Foredeep took place in the Wallachian (intra-Pleistocene) phase, and was characterised by the halokinetic processes involving the Lower Miocene salt deposits. As a result, four regional diapiric folds alignments, with various piercing stages of the salt were built up.

Two of these alignments i.e. Gura Ocnitei – Moreni – Baicoi – Tintea (“exaggerated diapirs”) and Bucsani – Aricesti – Ceptura – Urlati (“attenuated diapirs”) had a particular importance in the hydrocarbon entrapment.

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HYDROCARBON FIELDS IN THE EASTERN CARPATHIANS

Within the Eastern Carpathians, Parschiv (1979), B. Popescu (1995) distinguished 3 subunits:1. Paleogene Flysch Subzone2. Miocene Moldavia Subzone3.Mio-Pliocene Muntenia Subzone (Diapir Folds Zone)

Paleogene Flysch Subzone (Moldavides – Tarcau Nappe and Marginal Folds Nappe)Area – 9500 km2

Number of hydrocarbon structures: 27.Main source rocks: dysodilic shales and menilites (Oligocene)Main rocks having reservoir qualities: sandstones (Oligocene, Kliwa Sandstone Formation). These rocks present the following characteristics:

- porosity: 10-14%;- permeability: 2-100 md- pay horizons thickness: 20-30 m

Main types of traps: structural: normal and faulted anticlines, and scale folds. Average sizes of the structures:

a. Areas: 3-6 km2

b. oil-in-place: 25-150 MMbblInitial average production per well/day 40-600 bblPay formations: Oligocene

Miocene Moldavia Subzone Area – 2500km2

Number of hydrocarbon structures: 5.Main source rocks: dysodilic shales (Oligocene), blackish shales (Middle Miocene)Main rocks having reservoir qualities: sandstones and sands (Oligocene, Middle Miocene). These rocks present the following characteristics (average values):


Main types of traps: structural: normal and faulted anticlinals, and scale folds.Average sizes of the structures:

a. Areas: 1-2 km2

b. oil-in-place: 16-32 MMbbl Initial average production per well/day 16-40 bbl Pay formations: Paleogene and Miocene in Foredeep area of the Eastern Carpathians. Cretaceous and Miocene in the Moldavian Platform.

Mio-Pliocene Muntenia Subzone (Diapir Folds Zone)- Upper Mollase, External Foredeep

Area – 3000km2

Number of oil and gas fields: 38.Main source rocks: dysodilic shales (Oligocene), blackish marls and shales (Middle Miocene)

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Taste Oil and Wine – Field TripMain rocks having reservoir qualities: sands and sandstones (Oligocene, Burdigalian, Sarmatian, Meotian, Pontian, Dacian, Levantine). These rocks present the following characteristics (average values):


Main types of traps: structural: normal and faulted anticlines in relation with saliferous diapirism, and pinch outs, unconformities.Average sizes of the structures:

a. Areas: 6-12 km2

b. oil-in-place: 50-350 MMbblInitial average production per well/day 35-400 bbl Pay formations: Oligocene, Miocene and Pliocene.

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HADES VS. OILMANS (THE TASTE OF OIL)

FIELD TRIP ITINERARYThis journey area of interest is represented by the south-eastern flank of the Eastern

Carpathian belt.Everything you will witness in this trip is but a fade image of the complexity of the

geological, geographical, cultural and spiritual space which led to what Romania stands for today. The combination between human, natural and spiritual resources belonging to the north-eastern part of Muntenia is far deeper than what the eye of the ordinary tourist can perceive. Open the gates to your heart, faith and knowledge for each moment you will spend on this journey into petroleum history, geology and human communication.

“Taste Oil and Wine” Field trip

Timetable

Departure: Bucharest - Hilton Hote, 08:30

Bucharest - Urziceni - Buzau - Berca 08:30 – 11:00

Stop 1 Berca –Arbanasi Oilfield

Visit to the Mudy Volcanoes (Paclele Mari and Paclele Mici), 11:00-12:15

Berca - Cislau - Chirilesti 12:15 – 13:00

Stop 2 Chirilesti-Valea Rea

Upper Kliwa Outcrop - (Oligocene –Lower Miocene) 13:00 – 13:15

Chirilesti - Cislau – Valenii de Munte 13:15 – 13:45

Stop 3 Valenii de Munte - Free Time 13:45 – 14:45

Valenii de Munte - Ploiesti 14:45 – 15:15

Stop 4 Ploiesti

Visit to the National Oil Museum 15:15 – 16:45.

Ploiesti - Boldesti 16:45 – 17:15

Stop 5 Boldesti – Seciu - Boldesti Oilfield 17:15 – 17:30

Seciu wine cellar - Festive Dinner 17:30 - 20:00

Seciu – Ploiesti - Bucharest 20:00 - 21:30

Arrival: Bucharest Hilton Hotel, 21:30

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Stop descriptions

Stop 1 - Berca – Arbanasi Oilfield – Mudy Volcanoes

The structural Berca – Pacle - Beciu – Arbanasi alignment is developed along approx. 30 Km within the Subcarpathian Nappe and it is constituted of an anticlinal fold longitudinally and transversely tectonized through a fault system which makes that the relation between the structure flanks differs from one zone to another.

In the axial zone of the fold, Meotian and Sarmatian sedimentary deposits outcrop.

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Fig 8. Berca –Arbanasi BlockGeological map 1:200.000 RGI (fragment)

Fig 9. Berca – Arbanasi structure Geological Sketch map

Taste Oil and Wine – Field TripThe drilled wells (the deepest is over 3330m) cross a succession of beds belonging to

the Sarmatian, Meotian, Pontian, Dacian and Romanian. The lithological bed succession comprises more arenaceous levels than the adjacent areas (Moreni, Boldesti); the Meotian includes 27 sand levels among which most of them are productive. The Meotian hydrocarbon accumulations are accommodated in a number of sand beds different from one block to another. The nature of the fluids in the accumulations and their distribution within the alignment are different; the eastern flank is productive in all sectors of the structure (with oil, with or without primary gas cap and more rarely free gas), while the western flank is producing only at Pacle and Beciu (oil with primary gas cap and free gas).

The existence of numerous faults as well as the outcropping or the very high structural position of the hydrocarbon-satuarted Meotian deposits led locally to the partial deterioration of the conditions of fields sealing. The longitudinal and transverse

fault system created pathways of hydrocarbon (especially gas) migration to the surface, what brought about the occurrence of the spectacular phenomenon of Mudy Volcanoes. Along their way to the surface, the gas and the formation water drive the pelitic material and form mud which “erupts” in the area, in a few spots.

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Taste Oil and Wine – Field TripThe phenomenon of

the Mud Volcanoes crops up in a striking way close to Berca, at Paclele Mari and Paclele Mici. This area has been included in the list of the areas protected in Romania.

The geological and botanical reservation Mudy Volcanoes covers an area of approx. 30 hectares and comprises two areals: Paclele Mici and Paclele Mari

The Paclele Mici plateau represents a 9.4 ha natural reservation ever since 1924. The object of the

protection is the landscape displayed by the relief and the presence of two halophile plant species -Nitraria schoberi and Obione verrucifera.

At Paclele Mici, there is the largest number of volcanoes having cones, craters with highly varied sizes as well as complex morphology, on the one hand resulted from the mud accumulation and on the other hand by rain water streaming.

The volcanoes occur in groups of 3-5 units being of 2-8m high, with craters of 10-100cm diameters wherefrom viscous mud comes out, flowing as tongues which reach 20-50cm in length.

Paclele Mari is situated at a few kilometers to the north-east. The name is connected to the very large sizes of three main volcanoes having diameters of over 100m, which are lying in the centre of the plateau. The flanks of the cones are very widely spread,

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Taste Oil and Wine – Field Tripseveral cones of secondary volcanoes and long violet-blue mud tongues occur onto the former. The external half of the plateau is fragmented by ravines, torrents, developing scenery of badlands. The natural reservation covers an area of 19.6ha.

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Taste Oil and Wine – Field TripStop 2 – Valea Rea (Chirilesti) – Kliwa Sandstone Outcrop.

In Chirilesti locality, on the left of the nr.10 National Road (Buzau – Brasov), the Upper Kliwa Sandstone outcrops in an abandoned quarry.

Geotectonic setting is represented by Eastern Carpathians, Tarcau Nappe, Colti- Rea Valley Facies (Badescu, 1999)

Stratigraphy and AgeUpper Kliwa Sandstone

is Aquitanian in age. At the base, there are Podu Morii Strata, whereas at the upper part, the Dysodile Shales and Upper Menilites.

LithologyOn the reverse flank of a

fold dipping southwards, there are sandstone sequences

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Fig.11 Upper Kliwa Sandstone at Chirilesti, Rea Valley

Fig. 10 Upper Kliwa Sandstone - Buzau ValleyGeological map sc 1:200.000 IGR (fragment)

Taste Oil and Wine – Field Tripdisplayed in thick layers (sandy facies) and thin interbeds of dysodilic shales, (dysodilic facies), thin silts and sandstones, (Fig. 11).

Sandy FaciesBeds of decimetre and meter

thickness. The lateral continuity is good.

Grain-sizing belongs to the arenites’ range. Fine arenites are dominant, however, medium and coarse arenites are also encountered occasionally or even fine rudites in the base of some of the fining upward strata. The inner built structures are massive, fining upward and parallel

laminated (fig. 12). Within the base of the depositional units, there are linear vectorial structures of flute casts type (fig. 13) which points out an eastern source of the clastic material. The lower limits of the beds are net and flat as well as erosional, accompanied by mud clasts (fig. 12).

The upper limits are graded towards silts and dysodile interbeds. Cases have been encountered when the lower limits are graded from fine dysodilic facies. Petrographically, the arenites are quartzose and subquartzose

sandstones (>90% quartz), (Grasu, 1988, Anastasiu et al., 1999). Subordinately, there are encountered lithic sandstones within the base of some graded beds where the coarse arenites and fine rudites (granules) prevail consisting of anchimetamorphic lithoclasts of “Dobrudja-type” green schists (Fig. 14).

Dysodilic FaciesInterbeds of centimeter and

decimetre thickness, consisting of parallel laminated bituminous shales, millimetre-thick silts and centimetre-thick sandstones with asymmetric ripples at the top. There are cases when the whole dysodilic microsequence displays syn-depositional

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Fig. 12 Detail, arenitic and dysodilic facies. Mud clasts within the strata base

Fig. 13 Flute casts at the lower part of the strata.

Fig. 14 Lithoclasts of “Dobrudja-type” green schists within the base of sandy beds

Taste Oil and Wine – Field Tripdeformations, of convolute lamination type. The arenitic interbeds are also quartzose and subquartzose sandstones (Fig. 15).

Hydrodynamic interpretations:The massive sandy structures suggest

gravity flows of densely concentrated flows type where the clasts-supporting mechanism is mainly the particle collision and subordinately the turbulence. In case when the turbulent component prevails, the normal graded beddings and flute marks are formed at the bed base. The shales were formed by suspension settling, while the fine thin silts and arenites with top ripples resulted from traction processes. They can represent facies at the end of turbidity currents. The fact that there are load casts in the base of coarse sandstone strata points out a very high rate of sedimentation. The convolute laminations in the dysodilic facies suggest syn-depositional deformations along the slope - slumping.

Sequence and facies model The sequences are of a CUS (coarsening u) type, in case when progressive grading from

dysodilic facies to sandy facies takes place. The former are interpreted in the terms of turbidite lobes deposited at the slope base. The FUS (fining up) sequences, with an erosional base, suggest channel facies which supplied the turbidite lobes. Due to the very good lateral extension, these sequences have been interpreted in the terms of the arenitic turbidite systems having a linear source (Fig. 16), with the eastern source supported by both the paleocurrents measurements (Contescu et al., 1966) and the petrographic studies, given by the existence of lithoclasts of “Dobrudja-type” green schists (Anastasiu, 1984).

Economic BearingsThe high degree of lobes and

channels connectivity provides for a good quality of hydrocarbon reservoir rock. This quality is strengthened by good values of porosity (22-29%) and permeability (100-400 mD). As a matter of fact, the Kliwa Sandstone represents the main hydrocarbon reservoir of Tarcau Nappe. The hydrocarbon source is represented by the stratigraphic units of the Lower and Upper Dysodiles, with a high organic matter content.

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Fig. 16 Facies Model proposed for Kliwa Sandstone, arenitic turbiditic system, with eastern linear source in Anastasiu, et al., 1994


Stop 3 – Valenii de Munte – Free Time

Valenii de Munte is situated on the Teleajen Valley and surrounded by hills covered by forests and pastures. It is known thanks to the "Nicolae Iorga" Summer University which gathers scientists from Romania and abroad.

As regards the documentary attestation of this locality, some of the sources have dated it prior to 1400 under the name of Berevoieşti, but the most proofs exist for documentary attesting in 1431 through a deed issued by the ruler Dan II, wherein it is mentioned as a fair and customs area.

In the 19th century, Văleniul becomes a blooming town, as an important customs point along the road connecting Ploieşti to Braşov through Bratocea pass.

The town was chosen as permanent residence by the historian Nicolae Iorga in 1907, he established there, in 1908, the “Summer People’s University” – a place “of free tuition, altogether independent from the strictness of the scholastic regulations” (newspaper “Ziua” [The Day] dated 8 December 1937).

The house where Nicolae Iorga lived, now being “N. Iorga Memorial Museum”, discloses to the visitor the great man’s taste for the autochthonous folk creation. The exhibits in the museum: massive wooden furniture, carpets, paintings, personal belongings of the learned man restore the

genuineness of the scenery wherein the professor Iorga had thought and created his vast works.

The establishing of the “Religious Art Museum - Nicolae Iorga" in Valenii de Munte, located in the former building of “National and Ethical Missionary School - Queen Mary”, is related to the name of the great scholar. The Missionary School functioned during 1923 – 1940 in one of the oldest buildings at Valenii de Munte town, built in the 18th

century, in the style of the epoch houses specific to the Subcarpathian zone. The building lodges a valuable patrimony of icons, old religion books, silver ware and priests’ robes.

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Nicolae Iorga (1871 – 1940)

Nicolae Iorga Memorial Museum

Religious Art Museum


A museum probably unique in the world is at Valenii de Munte, it is about “Natural Sciences Museum – Plum-tree Growing”, dedicated to the culture of the plum-trees and manufacturing of the plum brandy.

Each year, at the end of the last week in October, at Valenii de Munte, the “Autumn Feats” are celebrated, an ample cultural-economic event where a special place is held by the manufacturing of

Bacchic beverage – plum brandy much loved by both the local inhabitants and the tourists who come here. Guests from everywhere can enjoy the agricultural-industrial goods fair, folk art and handicraft wares exhibitions, folk shows, competitions, dancing evening parties and of course; plum brandy tasting.

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Plum tree Culture Museum


Stop 4 – National Oil Museum - Ploiesti

In 1957, at the same time with the Romanian oil industry hundredth anniversary, it was decided the setting up of an oil museum, located in Ploiesti, city well-known as capital of the “black gold”..

In 1959, to the museum was allocated the building of the former night sanatorium of Refinery 1 (Astra), starting the acquisition of documents, photographs, artifacts, the initial thematic project following to reflect the development of our oil industry from the point of view of technical progress, work and living conditions of oil workers.

At its maturity age – 45 years – National oil museum unique in Romania and one of the few in the world has the honor of illustrating the history of Romanian oil industry, of oil science and technique, of the life of personalities and the events that represented the most important branch of Romanian economy.

Since 1994, the National Oil Museum has belonged to “Regia Autonoma” of Petroleum "PETROM" R.A. Bucureşti. Nowadays, the museum is under the authority of SC PETROM SA Member of OMV Group.

The Museum Building is included in the list of the historical monuments. The themes of the museum include the

following aspects: The history of oil exploitation and

revaluation, legal issues, social and political issues generated by this industry branch;

The beginning and the development of geological research in Romania;

The evolution of the equipment for drilling, extraction and oil processing;

The technology of drilling and oil extraction.Based on this themes, the basic

exhibition has been organized which is displayed in a hall with an area of 500 sq.m, exhibiting documents in original and in facsimile, geological maps, specialized technical documentation, photos and models reproducing specific equipment in the oil field as well as various technological processes.

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National Oil Museum - Ploiesti

Bustenari Oilfield 1929

Ancient Oilmans - 1910

Taste Oil and Wine – Field TripA second displaying area consists of a park of equipment and machinery - exhibits,

where there is displayed various equipment used to the extractive and processing industry, all being at least 60 years old.

Through years, by the help of the oil sector enterprises, the museum managed to gather an impressive patrimony dowry. Presently, this represent over 11000 inestimable goods – out of which 10 of an exceptional value proposed to be part of the “thesaurus”, admired by more than a million Romanian and foreign guests that enjoyed our hospitality.

The most important wealth is represented by the equipment – hoists, mud pumps, PH, rotary tables, tools older than 100 years.

“Toba de lacarit” - Ancient traditional oil extraction equipment – unique artifact dated 1870, the oldest exhibit;

Tescani type Friction -1895; Bernhardt Unit, mobile installation with animal traction, instrumentations - 1915, “Steaua

Romana”; Peine-Lemoine Holt, device for poles sets maneuvering in drilling process - 1930,

Original and rare exhibits of world oil techniques; “Hecna cu cai” scale model, manual equipment for exploiting oil from wells,

wells that reached the incredible depth of 320 m, the scale model being presented in the museum’s yard as a relic of an ancient time (the climax of the manual technique)

Other exhibition spaces are proud to hold original documents or copies, photographs of

inestimable value, geological maps, and old specialty books: Cucu Starostescu – “Petroleum” -1881, the world’s first specialty book; The first courses’ handbooks of the Bridges and Roads School, 1930-1935; Collection of Oil Gazette – In Romanian and French, 1900-1948; Functional scale models, dioramas, collection of oil lamps, water color paintings signed by Otto Barabas;

Should be mentioned some of the well known personalities of oil sector: Gregoriu Ştefănescu, Grigore Cobălcescu, Ludovic Mrazec, Valeriu Patriciu – in the field of geology; Ion Tănăsescu, Virgiliu Tacit, Ion Basgan, Andrei Drăgulănescu – in the field of drilling and extraction; Lazăr Edeleanu, Nicolae Debie – in the field of refining and petrochemicals.

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“Hecna cu cal” (“Hecna” with horse) – sec. VIII

Gregoriu Stefanescu – Eminent Geologist

Vergiliu Tacit - patented the blow-out preventer

Taste Oil and Wine – Field TripThe museum organizes special events – symposiums, temporary exhibition, open

courses, oil related contests for students, meetings with former oil workers, documentation trips to the most important oil sites from Prahova County and from the country.

Museum institution cooperates with other museums, foundations, schools, universities, oil industry companies, central and local authorities, ministries and so on.The National Oil museum belongs to the European oil museums network along together with museums from Germany, Norway, Hungary, Sweden, Poland and Austria. The main goal of this network is setting in line European programs in the view of solving some aspects related to patrimony inventory, legislation, conservation and restoration.

In the same time, the museum is founding member of the National Museums Network affiliated to Networking of European Museum Organizations (NEMO).

Generally, the supreme recognition of the activity is represented by the joy of having visitors – because they are those receiving information and sets up a bridge between events, past and present, they being the consumers towards our efforts are directed.

The museum waits for you to relive for a short time special moments of Romanian oil history, because as Nicolae Iorga said "the museum has to be a school of the taste and a school of taste history, … it has not only to be available to anyone but it have to offer a hand to anybody, for attracting him and keeping him as log as possible".

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Stop 5 Boldesti Oilfield – Seciu

The west-east trending Boldesti anticline is approx. 12 km long, 2.5 km wide, and together with Podenii Vechi anticline, is encountered in a lower structural position, so that Romanian deposits outcrop in its axis.

Morphologically revealed, the anticline is affected by a longitudinal fault along which the northern flank is sunk. A range of other longitudinal and transverse faults occur, however their importance is low within the trap configuration.

The structure includes oil and gas fields accommodated in formations belonging to the Pliocene (Dacian and Romanian) and Upper Miocene (Meotian) si Middle Miocene (Sarmatian).

The first information on the oil exploitation in Boldesti

area dates back ever since the 17th century. In 1901, it was drilled the first well in Pacureti area 28

Fig. 18. Boldesti Interpreted seismic line

Fig. 17. Boldesti areaGeological map 1:200.000 RGI (fragment)

Taste Oil and Wine – Field Trip(depth 469 m), in 1906, the first geological study is elaborated, while in 1907, at the 3 rd

International Petroleum Congress held in Bucuresti, a report is delivered on Boldesti – Seciu – Harsa area.

The gas fields pertaining to the Romanian and Dacian sequences were discovered after 1913.

In 1929, the 7AR- well was drilled onto Boldesti structure, at 1681 m final depth, which identified the first reservoirs at the Meotian level. The well yielded with an initial flow rate of 140 t/day.

In 1933, a European record is established through drilling the deepest well at that time. The Well 1-Creditul Minier reaches the extraordinary depth of 2540 m, it extends to the east the Meotian reservoirs, wherefrom it yields with initial flow rates of 384 t/day.

The oil accumulations at the Sarmatian level are identified in 1949 – 1950, when the 700-well is drilled which reached the depth of 3033 m. The well production started with an initial flow rate of 260 t/day, now it is producing approx.3.5t/day. The cumulated production of this well exceeds half million tons of oil.

The activities of exploration and identifying the hydrocarbon-bearing fields pertaining to Boldesti structure were carried out by stages of works. The drilled wells penetrated in succession the Pliocene (Romanian, Dacian), Pontian, Meotian,, Sarmatian and a part of the Upper Burdigalian.

The Romanian consists of marl and shale interbeds. The sands, separated in a few packages (15 ones in the apex zone of the structure), exclusively contain gas.

The Dacian is 250 – 300m thick and consists of sands with interbeds of marls, shales and coals. The sand levels were separated in 10 gas-saturated packages in the structurally uplifted blocks.

The content of Dacian and Romanian gas is over 99% methane.The Pontian is dominantly pelitic and it represents a good seal of the Meotian

accumulations.

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Boldesti Seciu Landscape – Otto Barabas

5 Well - Boldesti Oilfield 1929

Taste Oil and Wine – Field TripThe Meotian is approx. 400m thick and consists of marls with sand interbeds. The

Meotian sands were separated in 6 complexes, out of which three complexes are oil-saturated and three ones are saturated with gas and sometimes with oil.

The Sarmatian is represented by an alternation of sands and marls with interbeds of conglomerates and oolitic sandstones belonging to the Volhinian and Bessarabian. The sands were separated in five complexes. The oil is accumulated in two of these complexes, which exhibits an unconformable character, showing intraformation transgressive moments.

Thus, Boldesti structure accommodates Sarmatian oil accumulations, in tectonically closed traps (onto faults) and on stratigraphic unconformities.

The Meotian entraps oil accumulations with primary gas cap, whereas the Dacian and Romanian contain gas, only. The traps are structural, stratiform, arched, affected by faults.

Generally, the strata thickness ranges from 2.5 m to 23 m. The porosities vary between 18 and 25%, 27 – 31% pore water saturation, and the oil gravity is 0.840kgf/dc3.

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DIONISOS VS. OILMANS (THE TASTE OF WINE)

No comment!

The trip actually comes to an end here. From now on, the travel back to our homes will be for each of us an occasion to think upon what you have seen and learned, an opportunity of finding challenging topics of studying, of gathering more and more the relationships within this remarkable team who means the „Oilmen”.

The organizing team thanks you for participating in the Field Trip.

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SELECTED BIBLIOGRAPHY

CIULAVU D., DINU C., CLOETINGH S. A. P.L. 2002. Late Cenozoic tectonic evolution of the Transylvanian basin and northeastern part of the Pannonian basin (Romania): Constraints from seismic profiling and numerical modeling, EGU Stephan Mueller Special Publication Series, 3, 105–120

ANASTASIU N., 1984, What are the "green clasts" of the Carpathyan Flpsch? - a petrographic, reconsideration, Rev. roum., geol., geoph., gheogr., 28, p.51 - 60;

ANASTASIU N., POPA, M., VÂRBAN B.L., 1994, Oligocene turbiditic sequences of the East Carpathians (Romania): facies analysis, arhitecture and cyclic events. St. cercet. geol. geofiz, geogr. Seria geol. 39:p. 35-43.

ANASTASIU N., POPA. M., VÂRBAN B.L., DERER C., ROBAN R. D., 1999, The East Carpathian Reservoir Rocks - Kliwa Sandstone Formation. Geological Report, Bucharest, University of Bucharest, unpublished data.

BADESCU, D. 1999, Modelul structural al zonei externe a flişului din Carpaţii Orientali) partea centrală şi nordică) şi paleogeografia palinspastică la nivelul Senonianului şi Paleogenului. Archive of Faculty of Geology and Geophysics, University of Bucharest, 249 p;

BUTAC, A., DESEANU, D., DOBRE, S., GEORGESCU, C., GRECU, D., GHIRAN, M., POPESCU, M., SERINI, V., SINDILAR, V., STEFANESCU, M., ZAHARESCU, P., 1997, East Carpathian Bend Area, Romania: Oligocene – Pliocene Source Rocks, Reservoirs and Hydrocarbon Fields. AAPG International Conference & Exhibition, Vienna ’97. Trip #10 Field Trip Notes.

BUTAC, A., DINU, C., GRADINARU, E., OLARU, R., SERINI, V., SINDILAR, V., TAMBREA, D., 1998, Dobrudja and East Carpathian Bend Area, Romania. 3rd International Conference on the Petroleum Geology and Hydrocarbon Potential of the Black and Caspian Seas Area, Neptun 1998 Field Trip Guide Book.

CONTESCU, L., JIPA, D., MIHAILESCU, N. AND PANIN, N., 1966, The internal Paleogene flysch of the eastern Carpathians; paleocurrents, source areas and facies significance. Sedimentology, 7, 307321.

GRASU C., CATANĂ C., GRINEA D., 1988, Flişul carpatic. Petrografie şi consideraţii economice. Ed. Tehnică., 208 pp.

MAŢENCO, L. AND BERTOTTI, G., 2000, Tertiary tectonic evolution of the external East Carpathians (Romania): Tectonophysics, v. 316, p. 255-286.

OLARU, R., ROBAN, R., 2007, Getic Depression Field Trip, Guide Book, E&R PETROM June 7 – 9, 2007.

PARASCHIV, DUMITRU, 1979. Romanian oil and gas fields, Studii Tehnice şi Economice, 13: 382.

SĂNDULESCU M., 1984, Geotectonica României, Edit. Tehnica, Bucureşti, 320 pp.

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SĂNDULESCU, M., 1988, Cenozoic tectonic history of the Carpathians, AAPG Mem 19.

SERINI, V., POPESCU, M., 2006 Carpatii Orientali – Zona de Curbura, Prezentare Geologica – Ghidul Excursiei E&R PETROM 26 – 27 Mai 2006.

TĂRĂPOANCĂ M., 2004, Architecture, 3d Geometry and Tectonic Evolution of the Carpathians Foreland Basin, PhD, Netherlands Research School of Sedimentary Geology (NSG), 120 p

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