carboniferous black-shales and shale-gas...

CARBONIFEROUS BLACK-SHALES and SHALE-GAS POTENTIAL

in SOUTHWESTERN PORTUGAL

AAPG – Europe Region Annual Conference & Exhibition Post-Conference Field-trip 20th -21st May 2015

Paulo FONSECA Nuno PIMENTEL

Rui PENA DOS REIS Gabriel BARBERES

Carboniferous Black-Shales and Shale-Gas Potential in Southwestern Portugal

Paulo Fonseca Nuno Pimentel

Rui Pena dos Reis Gabriel Barberes

Field Trip Guide

ISBN : 978-989-20-5741-5

CARBONIFEROUS BLACK-SHALES and SHALE-GAS POTENTIAL IN SOUTHWESTERN PORTUGAL

This field trip will address the characterization and shale-gas potential of Carboniferous units in southern Portugal.

Most of the trip will be along wild coastal cliffs and beaches of the Southwest Coast Natural Park (PNSACV). We will look at deep marine turbiditic sequences, containing black-shales, affected by the variscan orogeny and low-grade metamorphism. Maturation and deformation issues are therefore crucial and will be discussed.

We will also look at the Mesozoic cover, namely the impressive Carboniferous-Triassic unconformity (Telheiro beach) and Jurassic limestones (Carrapateira beach) which may eventually act as potential reservoir units for the Paleozoic gas. The trip will end with a short stop at Ponta da Piedade, with karstic cliffs, natural grottoes and arches.

Main topics to be adressed:

Carboniferous black-shales – lithostratigraphy, source-rock potential, maturation and deformation.

Mesozoic cover - reservoir potential of Triassic red-beds and Jurassic dolomites.

Hydrocarbon potential – unconventional and conventional, onshore and offshore, Algarve and Alentejo basins.

LIST OF PARTICIPANTS

Paulo Bizarro , Partex Oil and Gas

Arkadiusz Buniak, ORLEN Upstream Ltd.

Bizhu He, Chinese Academy of Geological Sciences

Roger Higgs, Geoclastica Ltd.

Nuno Ines, Partex Oil and Gas

Fraser Keppie, Nova Scotia Department of Energy

Piotr Krzywiec, Institute of Geological Sciences, PAS

Carolina Libório, Galp Energia

Gil Machado, Galp Energia

Luca Mancinelli, Trinity College Dublin

Mariusz Paszkowski, University of Silesia

Magdalena Piatkowska, ORLEN Upstream Ltd.

Agnieszka Pisarzowska, Institute of Geological Sciences, PAS

Maciej Rybicki, University of Silesia

Justyna Smolarek, University of Silesia

Jaroslaw Zacharski, ORLEN Upstream Ltd.

1

DAY 1

Lisboa - Grândola (2 hours drive, mostly highway)

STOP 1 – Serra de Grândola

Introduction - regional geology. Mértola Formation

STOP 2 - Cabo Sardão

Black-shales of the Mira formation

STOP 3 - Monte Clérigo

Black-shales of the Brejeira formation

LUNCH - Monte Clérigo beach

STOP 4 - Arrifana beach


STOP 5 – Bordeira

Black-shales of the Brejeira Formation

STOP 6 – Castelejo


Dinner & Overnight - Hotel Memo Baleeira (Sagres)

DAY 2

Breakfast at 8.00, Check-out at 8.30h

Hotel – Carrapateira (20 min drive)

STOP 7- Carrapateira

Mesozoic cover of the Carboniferous basement

STOP 8 - Telheiro

Paleozoic – Mesozoic unconformity

LUNCH - Bag-lunch close to Sagres

STOP 9 – Sagres

Jurassic dolomites

STOP 10 – Lagos

Tertiary karstified cover

Lagos-Lisboa (3 hours drive, highway)

TIDES LOW HIGH 20th May – 10.40 (0.64) and 17.00 (3.50) 21st May – 11.10 (0.79) and 17.35 (3.35)

ITINERARY

2

STOP 1 Grândola

- Sines

STOP 2 Cabo

Sardão

STOP 3 Monte Clérigo

STOP 4 Arrifana

STOP 5 Bordeira

STOP 6 Castelejo

STOP 7 Carrapa-

teira

STOP 8 Telheiro

STOP 10 Lagos

Tertiary

Coastal Abrasion &

Sedim.Cover (70m)

Coastal Abrasion Platform

(40m)

--

Coastal Abrasion Platform (100m)

--


(80m)


(20m)


(80m)

Emersion Karstif. Infill

Mesozoic

Uplift and erosion

Uplift and erosion

Uplift and erosion

Uplift and erosion

Uplift and erosion

Uplift and erosion

Uplift and erosion

Trias-Jura subsidence

Uplift and

erosion

Late Carbonifer. deformation

Gentle folding

Tabular & gentle folding

Intense Folding

Tabular & gentle folding

Folding and

Thrusting

Tabular + Intense folding

Metamorf. basement

Metamorf. basement

--

Carbonifer. sedimentation

Moscovian

Serpukhovian

Shales & Greywackes

Mértola Fm

Black- Shales Mira Fm

Black- Shales

Brejeira Fm

Black- Shales

Brejeira Fm

Black- Shales

Brejeira Fm

Black- Shales

Brejeira Fm

Basement

Basement

--

STRUCTURE OF THE FIELD-TRIP OBSERVATIONS

3

LISBOA

PORTUGAL SPAIN

MOROCCO

LAGOS

ARRIFANA

CARRAPATEIRA

CASTELEJO

Monte CLÉRIGO

SINES

CABO SARDÃO

SAGRES

FRANCE

This field-trip will take us from Lisbon to the southern coast of Portugal, mostly along the Atlantic coast. All the stops will be on the seaside and inside SW Coast National Park (PNSACV), which extends from Sines to Sagres.

Most of this atlantic coast corresponds to vertical cliffs cut on Carboniferous black-shales, with the exception of some Mesozoic cover outcrops. Our overnight will be in Sagres, a former fishermen village, now a place for summer holidays and nature week-ends.

4

This field-trip will be focused on Carboniferous units of the Southern Portuguese Zone (SPZ) in SW Iberia. These units are part of the External Thrust Belt of the Ibero-Armorican Arc. Its geodynamic equivalents may be found in SW Ireland SW England and Rhenish Massif. In SW Iberia the Gondwana terranes are represented by the Ossa-Morena Zone, which contacts with the SPZ by the subduction-related Beja-Acebuches ophiolithc complex (BAOC).

WEIL ET AL., 2009 http://jgs.lyellcollection.org/content/167/1/127/F1.large.jpg

5

The Mértola, Mira and Brejeira Fms and its structures may be identified by its Total Radioactivity (ng/h) variations (Aerial Gamma Ray Spectrometry, collected by RioTintoZinc (1991), courtesy of LNEG).

The Baixo Alentejo Flysh Group (BAFG) is composed of three different Formations, considered to be diachronic. They represent a few kms of accumulated turbiditic deposits whih are considered to be SWwards increasingly: i) younger; ii) more distal and finner-grained; iii) thicker.

The proportion of greywackes and shales varies accordingly and therefore it may be considered that the Brejeira Formation is the most promising in terms of black-shales accumulated thicknesses, although organic-rich facies are present all along this Flysh sequence.

The BAFG covers the Volcano-Sedimentary Complex and the organic-rich Paraíso Formation, part of the Iberian Pyrite belt.

Tertiary

CARBONIFEROUS BLACK-SHALES - THE BAIXO ALENTEJO FLYSH GROUP

6

PQ

Late Devonian

VS

Early Carboniferous

LATE CARBONIFEROUS

Mauritania Iberia

? ?

LATE CARBONIFEROUS – EARLY PERMIAN COLLISION AND INTENSE DEFORMATION

N

S

Brejeira Fm

Mira Fm Mértola Fm

LATE PALEOZOIC REGIONAL GEODYNAMIC EVOLUTION OF SOUTWESTERN IBERIA Fonseca et al., 2015, (unpublished)

?

?

VS – Volcano-Sedimentary Complex

PQ – Phyllito-Quartzitic Group

7

Aljezur

Carrapateira Odemira Aljustrel

VS+PQ PL

SW Mira Mértola Brejeira

24.7 % SHORTENING due to folding

18% SHORTENING due to thrusting 36.3 % SHORTENING due to folding

DEFORMATION AND

SHORTENING in the SOUTHERN

PORTUGUESE ZONE

(in BOLACHA, 2014)

PL – Pulo do Lobo Formation; VS – Volcano-Sedimentary Group; PQ – Phyllito-Quartzitic Group; SW – Southwest Group

NE SW

97 km

27 km

70 km

8

STRUCTURAL LEVELS AND DEFORMATION The concept of structural level (as defined by Mattauer 1973) is based on the observation that the style of deformation changes with depth due to a large number of constraints such as: changes in temperature, confining pressure (overburden), geometry and vicinity of major accidents (thrusts), etc. In a thin-skin deformation model as SPZ, with extreme plastic units (black-shales), the presence of very closed to major thrusts changes dramatically the style of the structural levels. Near the thrusts, structures become more pervasive and sub-vertical, with a large number of advanced faults and fractures. At SPZ this scenario generally occurs on top of isopach to slightly stretched (A style) folds. At the base of the section, far away from the main thrusts, the bedding and early fabrics are always recognizable, locally with gentle folds or locally overturned folds, with an axial planar schistosity present.

9

DEFORMATION and SHORTENING Compression and folding modeling indicates regional shortening values around 35%. Major Thrusts may be responsible for up to 18% shortening. Geometric reconstruction of foldings at outcrop scale (photos) shows shortenings up to 52 %.

39%

36%

52%

10

CARBONIFEROUS BLACK-SHALES AND SHALE-GAS POTENTIAL

Carboniferous accumulation of a few thousand meters of turbidites with some organic-rich layers has been followed by intense subsidence and overburden at the end of the Carboniferous. Most probably there has been abundant generation of hydrocarbons. Terranes collision promoted intense deformation, with folding and thrusting to the SW, throughout the early permian. Permo-Triassic times have witnessed mostly uplift and coeval erosion of up to 5 km (?). Since the Late Triassic, Pangea’s break-up and Atlantic opening, promoted extension, subsidence and development of Mesozoic basins on the western and southern borders of the Iberian Massif (Alentejo and Algarve basins).

The potential of the Southern Portuguese Zone Carboniferous units for shale-gas is, at the moment, a line of scientific research supporting a future exploration pathway. There are clear lithological and faciological indicators of good source-rocks, allthough the present-day outcropping TOC values are naturally low. Organic matter maturation attained gas-window and there are also clear indicators of hydrocarbon generation, with pirobetumen in many samples. Deeply buried gas accumulations have been identified in some mining exploration wells, aiming at the Iberian Pirite Belt massive sulphides of the Sub-Culm. Permian deformation may have disrupted the continuity and integrity of these accumulations, but it may also have preserved some tectonic blocks from deeper overburdens, bringing them upwards along large-scale thrusts.

11

UNCONVENTIONAL

HYDROCARBON

SYSTEM CHART

SEDIMENTATION OM ACCUMULATION

COMPRESSION & FOLDING

THRUSTS

HC GENERATION

UPLIFT & EROSION

POST-OROGENIC OVERBURDEN

TOC data are scarce and do not seem to be very promising. However, is must be noticed that these are present-day outcrop values. This means that we are dealing with residual values - generation attained the Gas-window and most of the original Organic Matter has allready been lost.

Over-maturation, related to greenshist metamorphic facies has been the main obstacle to consider these units as having some shale-gas potential. However, Vitrinite Ro% data show some interesting heterogeneities and values below 3.0 (dark blue) or 3.5 (light blue), partucularly in the SW sectors between Arrifana and Castelejo.

Black – McCormack et al, 2007 Yellow – Fernandes et al., 2012 Green – Partex/Repsol, 2013 Red – Partex/Repsol, 2013

12

MIRA Fm

MIRA Fm

BREJEIRA Fm

BREJEIRA Fm

Monchique intrusion

ALGARVE Mesozoic

Basin

Sagres

Cabo Sardão

Lagos

ALENTEJO Mesozoic

Basin (offshore)

SW IBERIA Southern Portuguese Zone

1

2

10

3

4

5

6

7

8

5 6 3 4 2

9

2

6 10

13

Pre-CULM

Oliveira et al., 1984 Geological Map 1:200.000

ARRIFANA

Mte CLÉRIGO

CARRAPATEIRA

3

4

5

6

7

8

9

14

Manupella et al., 1992 Geological Map 1:100.000

STOP 1 – SERRA DE GRÂNDOLA Introduction to Carboniferous shales

This stop shows the characteristics of the Mértola Formation, with a predominance of Greywackes and minor intercalations of black-shales.

Stratification shows large-scale folding with inverted short limbs and vergence towards SW. Thrusts to the SW may also be seen, indicating an overall compression with that orientation.

Further down the highway, towards West, the contact with the Mesozoic is exposed, showing Late Triassic redbeds, clays and CAMP-related volcanics, followed by a Jurassic carbonate sequence, part of the Alentejo basin. These units are mostly covered by Plio-quaternary coastal sands.

WSW ENE

WSW

Deformation style B

15

STOP 2 – CABO SARDÃO Carboniferous black-shales

These high cliffs show the main sedimentary characteristics of the Carboniferous sequence of the Mira Formation, with alternating greywackes and shales. These rhytmic deposits correspond to median to distal turbiditic facies.

Deformation is moderate, with mainly ondulated layers and some decametric folds, with a southwards vergence.

The clif is around 40 m high and is topped by a Plio-Quaternary marine abrasion surface with rounded pebbles.

White stork nests on sea cliffs are characteristic of this place a and unique feature worldwide.

Deformation style B

16

STOP 3 – MONTE CLÉRIGO Carboniferous black-shales

The cliffs at Monte Clérigo show a predominance of intensively folded black-shales.

Towards the base (closer to the beach) deformation is less intense, whereas towards the top (southwards and upwards) some incipient thrusting may be identified.

This outcrop shows that slightly different deformation styles may occur allmost side-by-side. This may be due to depth-dependent factors, but also due to major thrusting accidents.

These large accidents have been identified along this coast, putting in contact units with strikingly different deformation and maturation intensities, as well as units with biostratigraphic gaps as long as 15 My.

This fact has strong implications to thermal maturation, sampling, analysis and interpretation, within an exploration framework.

Deformation style B

ATENTION – Wet rocks covered by green algae are extremelly slippery !

17

STOP 4 – ARRIFANA Carboniferous black-shales

This bay exposes deposits from the Brejeira Formation, with black-shales and fine-grained greywackes.

Deformation is moderate, with large-scale ondulated folds, characteristic of deeper structural layers.

The cliff goes up to 100 m high, with a distinct abrasion surface. At the far-end horizon it is possible to see a lower surface, corresponding to the Mesozoic Carrapateira outlier (Stop 6).

A Deformation

style

18

STOP 5 – BORDEIRA Carboniferous black-shales

This small outcrop shows rich organic facies with apparently not very high maturation.

A big thrust is exposed on the left side, indicating that this deformation occured mostly in upper structural levels, related with the Late Paleozoic up-lift.

C Deformation style

19

This long outcrops extends from the Castelejo beach northwards, untill the Cordoama beach.

The Northern half exposes highly deformed black-shales and fine-grained greywackes, with complex folds and inverted polarities.

An important sub-vertical thrust, brings to contact the previously described layers and much less deformed tabular layers, exposed at the Castelejo beach. Thermal maturation seems to be lower in this southern sector.

STOP 6 – CASTELEJO Carboniferous black-shales

A C

20

Carboniferous basement U. Triassic redbeds

Middle Jurassic (?) dolomites

Basin’s tectonic border

7A - BORDEIRA BEACH On this western mostly Paleozoic coast, a Mesozoic outlier may be seen at the Carrapateira promontory. It corresponds to a downthrown block, with a clear tectonic eastern limit, preserving most of the Mesozoic sequence. This infill may be correlated with Alentejo offshore basin as welll as with the Algarve basin (only 20 km away).

N

STOP 7 - CARRAPATEIRA Mesozoic cover

ALENTEJO Basin

21

UPPER JURASSIC

Volcanic tuffs and breccias

Marly limestones (*dolom)

Limestones and Dolomites

Middle JURASSIC Dolomites

Lw JURASSIC Marls & dolomites

HETTANGIAN Red clays & marls

UPPER TRIASSIC Redbeds

7C 7A 7B 7C

7A

7B

Ribeiro et al., 1987 Geological Map 1:50.000

STOP 7 - CARRAPATEIRA Mesozoic cover

Along the Carrapateira promontory a Late Triassic to Late Jurassic sequence can be seen. This Mesozoic cover may eventually act as a conventional reservoir for Paleozoic sourced hydrocarbons, a play which has been successfully tested in other Portuguese basins (Upphoff, 2005)

Late Triassic redbeds are covered by Hettangian red clays and dolomites, followed by Early and Middle Jurassic carbonates with intense dolomitisation, ending with Late Jurassic marls.

Magmatic intrusions may be observed, mainly related to the Late Jurassic doleritic Alentejo-dyke.

N

1 km

7A – Bordeira beach 7B – Três Angras bay 7C – Amado beach

22

Kimmeridgian marls with Source-rock potential

7B - TRÊS ANGRAS BAY

Upper Jurassic interbedded limestones and marls at Três Angras.

Calciclastic marls and bioclastic limestones pass into interbedded grey marls and limestones, with some potential as source-rock. The uppermost limestone beds are rich in macrofossils including well preserved corals.

Vitrinite Reflectance studies point to an uplift of about 2 km, part of it from the Late Cretaceous to the Paleogene (Fernandes et al., 2013).

N STOP 6

CARRAPATEIRA

STOP 7 CARRAPATEIRA

23

Upper Triassic aeolian like redbeds

Hettangian red clays & dolomites

N N

STOP 7 CARRAPATEIRA N

S 7C - AMADO BEACH

The cliifs North of this beach expose the Upper Triasic red-beds, with alluvial-fan coarse lags and eolian-like fine-grained sands, covered by sabkha deposits. This pair of sands/clays may act as a Reservour/Seal for Paleozoic gas, as proven in the Lusitanian Basin.

Looking Northwards this sequence is interrupted by a magmatic intrusion related to the CAMP event.

Looking southwards, Carboniferous units appear again.

24

U.Triassic redbeds

Carboniferous folded metasedimentary basement

Hettangian red clays and marls

Pliocene marine abrasion surface

This major unconformity between Carboniferous shales and Triassic redbeds resulted from a long geological evolution: i) deposition of marine clays and sands in a distal turbiditic environment, c. 320 My ago; ii) intense orogenic subsidence, heating and ductile deformation (5km depth?), c.320-300 My: iii) post-orogenic uplift and erosion of 4.5 km (?), until exposure and weathering, c.300-230 My; iv) deposition of fluvio-aeolian sands (c.230 My) unconformably covering folded Carboniferous.

N

STOP 8 – TELHEIRO Unconformity - Carboniferous

shales vs. Mesozoic cover

25

Carboniferous metasedimentary basement


U. Triassic redbeds Carboniferous

metasedimentary basement

U. Triassic redbeds



Quaternary consolidated aeolian dunes

Sinemurian dolomites

Pliocene abrasion surface S. Vicente

Cape

S N

STOP 8 TELHEIRO

26

Sagres is the “Promontorium Sacrum”, considered by the Romans as “the western end of the inhabited world”. This is a place with a tremendous historical importance. It was at least as important during the Age of Discovery as Cape Canaveral was during the early years of space exploration.

It was to this place that Prince Henry the Navigator, came in the 15th century to work on his obsession to push back the frontiers of the known world, and opened the phase in Portuguese history called The Discoveries.

STOP 9 – SAGRES Jurassic dolomites

N

1 km

Rocha et al., 1979

TELHEIRO

SAGRES

St. Vincent CAPE

These high vertical cliffs correspond to Lower Jurassic dolomites, which may act as conventional reservoir (both primary and fractured) for Paleozoic gas.

27

STOP 10 – PONTA da PIEDADE

This touristic spot shows well developed karstic erosion in Miocene limestones. After the Mesozoic infill of the Algarve Basin, intense inversion resulted in uplift and erosion during the Late Cretaceous and Paleocene in the present day onshore areas. Sedimentation resumed in Middle Miocene with deposition of rhythmic fossiliferous limestones and marls in coastal environments.

This coastal landscape is also a result of the the post-Miocene uplift of the Western Algarve during the Plio-Quaternary. Karstic features are partially filled up by Pliocene red sands, which after collapse of the karstic vertical wall give place to the present-day holes and arches.

Offshore, coeval formations may act as conventional reservoirs, sealed by Plio-Quaternary clays.

28

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29

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